Yet C i
oa “ ‘ y
« 7 ca ¥
ve fo ot
4 ale tet
J t ae
Creches
ra lee ae |
fe
ae ka dy
ype ee Pew
Te ee
bv
TR Le OS ee
be aed
y
Te ee
—
Ponty MeN
~
1S \CHiwea tart ated hal
i
" ete ibeobeibege w ee wte ty Welbe fhe tk tamndt
battle t hn AE tae 1 eres
‘ 1 lana the ‘ a:
ee ee MAL abet banter Rap how
‘ a AGN beth Dew beiesnegon
Hahah heb te a vee ey i " Dicthinll boris line
a . i} i 4 Sletten dw Hora tyes
Het dete RD vate dob he , a ee) a
tM Ke tbithokeg Morand
ie ee ee oe
bnitndl
a)
er) ayndd jon
iv y Vsirarta eth
, . tte We YAN a theater Ud 4
oe ‘ ;
‘ A Mette dbiotbe thsi
, 1 ‘ uid es wow
, oo " oh ‘ Wyo Pal thet , thet
1 Voweo oa ih a hy ee ee a ‘4 ‘ ie Vb ened ad
aol . o tot htt Holt ted Wott Bett
‘ \ on tay rr Pie ee ee ewe ce ‘ . ’ Fe doodin toe Potbet lh idedmih =
’ ‘ ‘ i g 4 oO ' * ,
4p Att mh ede tad tired An > Bh - Wohin ' ' :
’ ' A Nu ee a ' 4 we ‘
J he “ (ee nee | q ipa tee Vena Ab Corer ea)
a ' Ka Sots A 0
, i ‘ setae bm tata te Moat Wet Pi dot
« ci tose é “ “ vat Ltole “ fn bewoten
‘ ty ey ‘ ‘ i ‘ iat a '
4 A ~~ ae . 4 tan Pe Dnt ‘ ‘
‘ toteath 4 ‘ rn ‘ ‘ é
‘ any) " , ‘
‘ V lvsih * \ i ‘ Pa tnw
hoe ‘ Wd vedo ¥ j
‘ Lait hethowy bo . ’
j “ ‘ ” "
i q ‘ : “i
‘ : ‘ * " _
: eb
oe ae Te ie) Pome
Bie eee 2 Se
; ae a a “= , + 4 : RK
a Te om - 7 [en - -
a ¥ ; 7 =. 7 : 7 -
, Aa
mt I 738 ae aes bea = aa is 4
SereGanters, (att bei: B 842 ts 2
5, Ne ee ote ee
wAey At fap Ahi hieenss be Tes
N. ) THE
QUARTERLY JOURNAL
GEOLOGICAL SOCIETY OF LONDON.
EDITED BY
THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.
Quod si cui mortalium cordi et cure sit non tantum inventis herere, atque iis uti, sed ad ulteriora
penetrare ; atque non disputando adversarium, sed opere naturam vincere; denique non belle et probabiliter
opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant.
—Novum Organum, Prefatio.
VOLUME THE THIRTY-SEVENTH.
CULL "7 Visas ’
1881. KS
LONDON: LURE Ta
LONGMANS, GREEN, READER, AND DYER.
PARIS: FRIED, KLINCKSIECK, 11 RUE DE LILLE; F. SAVY, 24 RUE HAUTEFEUILLE,
LEIPZIG; T.O. WEIGEL.
SOLD ALSO AT THE APARTMENTS OF THE SOCIETY;
MDCCCLXXXI.
List
OF THE
OFFICERS
OF THE
GEOLOGICAL SOCIETY OF LONDON.
Present,
R. Etheridge, Esq., F.R.S.
Wice-Prestents.
John Evans, Esq., D.C.L., LL.D., F.R.S. Prof. J. Morris, M.A.
J. W. Hulke, Esq., F.R.S. H. C. Sorby, Esq., LL.D., F.R.S.
Secretaries.
Prof. T. G. Bonney, M.A., F.R.S. | Prof. J. W. Judd, F.R.S.
PForeiqn Secretary.
Warington W. Smyth, Esq., M.A., F.R.S.
Creasurer,
J. Gwyn Jeffreys, Esq., LL.D., F.R.S.
COUNGEIL,
H. Bauerman, Esq.
J Gwyn Jeffreys, Esq., LL.D., F.R.S.
Prof. J. F. Blake, M.A. Prof. J. W. Judd, F.R.S.
Prof. T. G. Bonney, M.A., F.R.S. Sir John Lubbock, Bart., M.P., F.R.S.
W. Carruthers, Esq., F.R.S. Prof. N. S. Maskelyne, M.P., M.A., F.R.S.
Prof. P. M. Duncan, M.B., F.R.S.
Prof. J. Morris, M.A.
R. Etheridge, Esq., F.R.S. J. A. Phillips, Esq., F.R.S.
John Evans, Esq., D.C.L., LL.D., F.R.S. F. W. Rudler, Esq.
Lieut.-Col. H. H. Godwin-Austen, F.R.S. | Prof. H. G. Seeley, F.R.S., F.L.S.
J. Clarke Hawkshaw, Esq., M.A.
Warington W. Smyth, Esq., M.A., F.R.S.
Rev. Edwin Hill, M.A. H.C. Sorby, Esq., LL.D., F.R.S.
W. H. Hudleston, Esq., M.A. H. Woodward, Esq., LL.D., F.R.S.
J. W. Hulke, Esq., F.R.S.
Assistant-Secretary, Librarian, anv Curator.
W.S. Dailas, Esq., F.L.S.
Clerk.
Mr. W. W. Leighton.
Librarp and fMuseum Assistant.
Mr. W. Rupert Jones.
TABLE OF CONTENTS.
ANDREWS, Rey. W. R. Note on the Purbeck beds at Teffont .... 251
BuakE, Rey. J. F. On the Correlation of the Upper Jurassic Rocks
of England with those of the Continent.— Part I. The Paris
erasOTPMn Obs NONOVIE hore cs sie oie eile sarees sino) o sie lel ei s'= sige e oie 497
Bonney, Rev. Prof. T. G. On the Serpentine and associated Rocks
of Anglesey ; with a Note on the so-called Ser pene of Porth-
TLE De 6 sin agibroidit: cid OxeRDON IG I ena EDs nee 40
On a Boulder of Hornblende Picrite near Pen-y-Carnisiog,
PMNS SVM Ee Petra Pela cio ah nei Stai's, hs = oie ois! at slausiia's: oe) sileyeie ele 5 « 137
Notes on the Microscopic Structure of some Anglesey Rocks 232
Bropis, Rev. P. B. On certain Quartzite and Sandstone Fossili-
ferous Pebbles in the Drift in Warwickshire, and their probable
Identity, lithologically and zoologically, with the true Lower
Silurian Pebbles with similar Fossils in the Trias at Budleigh
ACHE ORAM CM OTIGMILO 21) a ti c/s ta «aid eet olor Sv cack me wo elaieleres ee ene 430
Buckman, JAmzEs, Esq. On the Terminations of some Ammonites
from the Inferior Oolite of Dorset and Somerset ............ 57
Buckman, 8. 8., Esq. A descriptive Catalogue of some of the Spe-
cies of Ammonites from the Inferior Oolite of Dorset ........ 588
CatLaway, Dr.CHarites. The Archean Geology of Anglesey; with
an Appendix on the Microscopic Structure of some Anglesey
fvecuompy Eton |. (G. Bonney. (Plate VE)... 3... 210
The Limestone of Durness and Assynt.................. 239
CarPENTER, P. H., Esq. On two new Crinoids from the Upper
Chalk of Southern Sweden, GElater Valle arses crates seas oe 128
CaRRALL, JAMES W., Esq. Notes on the Locality of some Fossils
found in the Carboniferous Rocks at T’ ang Shan, China ...... 83
@orewerr, Dr. R. W. On Soil-cap Motion..............0.006: 348
Davis, JAMES W., Esq. Notes on the Fish-remains of the Bone-bed
at Aust, near Bristol, with the Description of some new Genera
207, Syoweresy (Celera 9.0.4 De i ee an nen nen 414
On Anodontacanthus, a new Genus of fossil Fishes from
the Coal-measures, with Descriptions of three new Species.
TElghe OCLL) Seis RRR See inns aioe a aeeientain oi ee 427
iV TABLE OF CONTENTS.
Page
Dawson, Dr. G. M. Additional Observations on the Superficial
Geology of British Columbia and adjacent regions............ 272
Dawson, Dr. J. W. Notes on new Erian (Devonian) Plants. (Plates
GHC a>. C U0) NA aim SAMmin norma oh aboDe do Gs dccooso on cor 259
Duncan, Prof. P. Martin. On the Coralliferous Series of Sind,
and its Connexion with the last Upheaval of the Himalayas.... 190
Dunn, E. J., Esq. Notes on the Diamond-fields, South Africa, 1880 609
Ecciss, James, Esq. On the Mode of Occurrence of some of the
Volcanic Rocks of Montana, U.S. AS. ee acer ee 399
ETHERIDGE, R., Esq. On a new Species of Zrigoma from the Pur-
beck beds of the Vale of Wardour; with a Note on the Strata
by the Rey. W. ER. ANDREWS 9 .0).)02 66 «elec ieee eee 246
. On Plant-remains from the Base of the Denbighshire Grits.
(Plate XOXW ies ot a ae oeacteio ravens one tiene te BPRS cc i50 6 490
Hicks, Dr. Henry. On the Discovery of some Remains of Plants
at the Base of the Denbighshire Grits, near Corwen, N. Wales;
with an Appendix by R. EruEripeGs, Esq. (Plate XXV.).... 482
Hotiinewortu, G. H., Esq. Description of a Peat-bed interstrati-
fied with the Boulder-diift at Oldham .....--.. 72 eeeeee 713
Hormss, T. V., Esq. The Permian, Triassic, and Liassic Rocks of
the Carlisle Basin. (Plate X05)... 3. oc). 9. 286
Jupp, Prof. J. W. On the Occurrence of the Remains of a Cetacean
in the Lower Oligocene Strata ofthe Hampshire Basin; with an
Appendix by Prof. BG. Simtiny Pues ts. ee eee 708
Krrpine, H., Esq., and E. B. Tawnry, Esq. On the Beds at
Headon Hill and Colwell Bay in the Isle of Wight. (Plate V.) 85
KEEPING, WALTER, Esq. The Geology of Central Wales; with
an Appendix on some new Species of Cladophora, by CHARLES
LAPWORTH, Hsq. (Plate VIL) 9.02.0. ee 141
KENDALL, J. D., Esq. Interglacial Deposits of West Cumberland
and North Lancashire. (Plate TMI)... co. a oe eee 29
LaPworTH, CHAR Es, Esq. On the Cladophora (Hopk.) or Dendroid
Graptolites collected by Prof. Keeping in the Llandovery Rocks
of Mid Wales. (Plate VIL)... ......522 08 oe 171
MackinTosu, D., Esq. On the precise Mode of Accumulation and
Derivation of the Moel-Tryfan Shelly Deposits; on the Discovery
of similar High-level Deposits along the Eastern Slopes of the
Welsh Mountains ; and on the Existence of Drift-zones, showing
probable Variations in the Rate of Submergence.............. 301
Moor®, Cuaruzs, Esq. On Abnormal Geological Deposits in the
Bristol District. 0 5.0.5. 620+ aes oe on ene 67
Owen, Prof. R. On the Order Theriodontia, with a Description of
a new Genus and Species (4lurosaurus felinus, Ow.). (Plate IX.) 261
Description of Parts of the Skeleton of an Anomodont
Reptile (Platypodosaurus robustus, Ow.). Part II. The Pelvis.
(Plate) ee oa eee oes 266
TABLE OF CONTENTS. Vv
Page
PaRKINSON, C., Esq. p Upper cope) and Chloritic Marl, Isle of
Ne Nee hea. ores wi sialcs PATS Ss Stowell aGocuarl Siw Beat 370
Puitiies, Joun ARTHUR, Esq. Note on the Occurrence of Remains
gigcecent Plantsiim row? Irom-0re. .32)) ines ce aes Soe wie ee if
. On the Constitution and History of Grits and Sandstones.
perma SPU Orme: Meoes uateape aldlai beets cal sky os altho sya) Gai io:4 vise ale «2 36s 6
REavDeE, T. MELLARD, Esq. The Date of the last Change of Level in
1 IDOE SIDTRG eo SiS es APO Come SEO ER cP ene BOR ran 456
RuTLeEY, FRanK, Esq. The Microscopic Characters of the Vitreous
Rocks of Montana, U.S. A.; with an Appendix by JAMES EccLEs,
IPT opm OL ALCP NO NG clare teccrs esol, oid agetd Sa cls aie ealocenepeianc ie ptt w ofiere, Sele 591
On the Microscopic Structure of Devitrified Rocks from
Beddgelert and Snowdon ; with an Appendix on the ae
Rocks of Skomer Island. ’ (Plate O05) ete Peet pn see En NO 403
SrEeey, Prof. H.G. On Remains ofa small Lizard from the Neo-
comian Rocks of Comén, near Trieste, preserved in the Geological
Museum of the University of Vienna. (Plate IV.) .......... 52
The Reptile Fauna of the Gosau Formation preserved in
the Geological Museum of the University of Vienna; with a
Note on the Geological Horizon of the Fossils at Neue Welt,
west of Wiener Neustadt, by Prof. Epwarp SvusEss. (Plates
ETT OO. Ae ee eee cheno PRS ee Pa aa art 620
Note on the Caudal Vertebra of a Cetacean discovered by
Prof. Judd in the Brockenhurst Beds, indicative of a new Type
allied to Balenoptera (Balenoptera Juddi.)... 1... cece ee eae 709
SHRUBSOLE, G. W., Esq. Further Notes on the Carboniferous
“PS ES YSIIEGISS J 5G hte Gasser Me NEy CRANE AEE 178
Sounas, Prof. W. J. On Astroconia Granti, a new Lyssakine Hex-
actinellid from the Silurian Formation of Canada ............ 254
On a new Species of Plesiosaurus (P. Conybeart) from the
Lower Lias of Charmouth; with Observations on P. megace-
phalus, Stutchbury, and P. brachycephalus, Owen ; accompanied
by a Supplement on the Geographical Distribution of the Genus
Plesiosaurus, by G. F. Wurpporne, Esq. (Plates XXIII. &
URN Pen cia ee ey ire ai Sia nah a tiene Rane! iz teieie dase the 440
Susss, Prof. Epwarp. Note on the Gosau Beds of the Neue Welt,
UE SDROMAY TENCI NGUSCAGCG. «206s syn ceunredials's a Se ds be eernae we 702
Tawney, EK. B., Esq., and H. Kreprne, Esq. On the Beds at
Headon Hill and Colwell Bay in the Isle of Wight. (Plate V.) 85
Ving, G. R., Esq. Further Notes on the Family Diastoporide,
Busk, § pecies from the Lias and Oolite. (Plate XIX.)...... 381
Silurian Uniserial Stomatapore and Ascodictya.......... 613
Waters, A. W., Esq. On fossil Chilostomatous Bryozoa from South-
west, Victoria, Australia. (Plates XIV—XVII.)............ 309
vi TABLE OF CONTENTS.
Page
Wutpporne, G.F., Esq. Tabular Synopsis of the Geographical
Distrbucion onthieyieleslosaursrar | easels eee is ciel aes tele ioe renner 480
WILLETT, Epear W., Esq., and Henry WILLETT, sq. Notes on
a Mammalian Jaw from the Purbeck Beds at Swanage, Dorset. 376
PROCEEDINGS.
Page
anual’ Reports. cecteeaela t reece) ite oe 8
duist of Horeien Miembersi). caer eerie eee 16
List of Foreign Correspondents .........-. +... eee eee eernneeee 17
List of Wollaston’ Medallists\2 72); oni... 0 0 -isie ere eeee 18
List of Murchison Medallists. 066.522 «joes aie eee 19
Taist of lyellt Medallists ie. se ieee ae eeeeeie 20
Mist ot Biesby Medallists) 2 ee retteeee 21
Mimancial Report. ce. cre crete peters ellie rie Rents sie “ag eae 22
Award of the Medals &. 0.05. 6 oie 1. sie she oes ile aie ketene ee 28
Anniversary Address... 2). ciel eee cine Cle elo eee 37
Donations to the Library (with Bibliography) .................. 244
Presentation of Portrait of William Smith? 2.05. oon 2
Haun, Dr. Otto. On Microscopic Sections of Meteorites ........ 7
Lones, F. D., Esq. On some Specimens of Diastopora and Stomato-
pora from the Wenlock Limestone. (Abstract.) ............ 2.39
Bequest of Drawings of Fossil Fishes by Sir Philip Egerton ... ni 241
LIST OF THE FOSSILS FIGURED AND DESCRIBED
IN THIS VOLUME.
[In this list, those fossils the names of which are printed in Roman type have
been previously described. ]
Name of Species. Formation. Locality. Page.
Incerteé sedis.
Tubutella ambig“ua .......csceceeceecees |Jurassic &c..,.... [pe Britain’ esse Pvt
PLANT.
Aitheotesta devonica. PI. xii. f. 14. \ | (Scotland ...... 306
Archeopteris, sp. Pl. xiii. f.19 ... | | New Brunswick 305
Asteropteris noveboracensis. PI. xii. | |
RNS e so inincio'rsiesivn's «see ce sciees New York ... 299
Cardiopteris eriana. P\. xiii. f. 18.. New Brunswick 305
Celluloxylon prim@vum ....0..ee0.00e- | | New York ... 302
CIOPLCTISN SD! gio cejsicess aise cetee eecie ss | . | New Brunswick 305
Cyciostigma affine. Pl. xii. f. 11, 12 p PSOE Bac sccu: 4 New York ... 301
Dicranophylium australicum. Pl. |
sai Te, Aa ee Australia ...... 306
Equisetides Wrightiana. Pl. xii. f.10,
[P| STG 15 7A Dee eee ee New York) .2: 301
Lepidodendron primevum. PI. xii.
RBSRPRRC Rae ons Sieacincencinieesedseonss ) \ New York ... 302
ue ematop ee, I STITHEIN Fagabeose WaleSiteces.c.8 494
a fier oeamnosa: 4 El xi. } Devonian......... New Brunswick 305
Pachytheca. P|. xxv. f.7-9 ........ Silurian sceece-e: Wealesm.css.cce: 483
SPONGIA.
Astroconia Granti ......... Gonocsdcdden UTTER ear apee | Camnada......... | 254
Vill FOSSILS FIGURED AND DESCRIBED.
Name of Species. Formation. Locality. Page.
C@LENTERATA.
(Hydrozoa.)
Acanthograptus ramosus. PI. vii. \ |
CBO ga cies sanceisiveisislncis sisters gaa femaees ( 174
Calyptograptus’? digitatus. PI. vii. | :
dees deaticoccingediansecucnanaeancenee 173
plumosus. PI. vii. f. 4.......... | 174
Die tyonema genome TL aL ( Llandovery ...... Central Wales {
Se Caneee weelseceiacuislemece aaeacieise es | 172
delicatulum. Pl. vii. f.2 ...... | | 172
DONUSLUNE aly neville gl gece eectye: el a alee
Odontocaulis Keepingii. PI. vii. f. 7) L| 176
ECHINODERMATA.
Antedon impressa. Pl.vi.f.8,9... |Upper Chalk ...| Sweden ...... 135
Mesocrinus Fischeri. PI. vi. f. 1, 2: |Planerkalk ...... SaMONYV sess 130
suedicuss Pl vie fade vasneeeoss Upper Chalk Sweden meee 132
PoLyzoa.
Ascodictyon radians «............+-+0. USERS A Sosecoe: Britain 618
Stellatum: cecjaddesc-cssrseneeene
Caberea rudis. PI. xviii. f. 86 ...... \ (| 322
Canda fossitis. Pl. xvi. f. 51, 52... 322
Catenicella alata. Pl. xvi. f.47, 49,
OOo Gos Hei aeons mee cece ee er 317
ampla. Pl. xvi. f. 46, 50...... | 317
cribriformis. Pl. xvi. f. 39... 317
elegans, var. Buskii. Pl. xvi. |
fA 2 AG ee one rae ee e 317
flexuosa. Pl. xvi. f. 40, 41 . 317
—— internodia. Pl. xvi. f. 78, 79.. 318
marginata. Pl. xvi. f. 44, 45.. 317
soliday selexvie isso Or re ; 318
Cellaria fistulosa. Pl. xiv. f. 1, 2, MMICBANS Goscesoe: se Australia
DOV cir eine Biaeataseiy Satara ea eee 319
qlouusosay abaleexivenie lon lezmee 321
— malvinensis. Pl. xiv. f.3...... 321
ovicellosa. PI. xiv. f. 4-6, Pl. |
NVI O Qiiciae ecseeaae tee ee coe 321
Cellepora fossa. Pl. xviii. f. 89 ... 343
UT ARTIS atic benconecebuebassoe | 343
SAS DE sSecece tat scrote ce eee eee 344
Cribrillina dentipora. P\. XY. 1 33. 326
suggerens. Pl. xvii. f. 75.2... 327
terminata. PI. xvii. f. és ey (| 326
Diastopora cricopora. P|. xix. f. 18-
2 ince dale nase echt Mone tenet ea eee Ooliter2 see Britaines cee 387
— oolitica. PI. xix. f. 11-14 386
es Ee a Britain &e. ... | 384
ventricosa. Pl. xix. f.15-17.. |Oolite ............ Britain’. 2.2.4.9: 385
FOSSILS FIGURED AND DESCRIBED. 1x
Name of Species. - Formation. Locality. Page.
Potyzoa (continued).
HEMESUCIIAS CLASS onc c.0 eevee. ca cseeee \
(| 186
DUMENSIS 55.25 sas ale sccco deen ig EST
—— membranacea..................005 Carbonif Britain , 181
== COS ee ee r |Carboniferous -.. race heey 183
=== GE 179
MOLY HOLAGA! 6.0 5os50cedeodeossecace ) 185
Lepralia cleidostoma, var. rotunda. \
Pls SOU, 1 Ee een ee are 336
corrugata. Pl. xvii. f. 60...... 339
monilifera, var. armata. Pl. xv. |
BPM ooo Sclch oaiacis vig ciencicanbawe's 335
spumulata. Pl. xvii. f. 87...... 335
Membranipora argus. PI. xiv. f. 20, é
BUN en oo Sahin tins chew eeaicerinn 24
GAME MOANA seo sicfoicie's saree <'s/ejeie as 323
cylindriformis. Pl. xvii. f. 74 323
concamerata. PI. xiv. f. 22, :
PME ie icticinc nts aceeiseddesuees 24
gemmara: Pl. xvi. f..95 ...... | 325
MCE AMER ees S oSaaiso idee gies 323
lusoria. Pl. xiv. f. 14, Pl. xviii.
if, eos soclgonoSO OER CHOEe Ronee ee eeenCe 324
— macrostoma. Pl. xiv. f. 18, 4095
tuaonicar | Ploxiv. £9) ..:...... 329
WVIGCTONONOPAUMUEA oo. ceccceccssaacess 326
Microporella enigmatica. Pl. xv.
i, 2D AD) cocc ene g eee ae eee 331
clavata. Pl. xviii. f. 84 ...... |
coscinopora, var. armata. PI. |
RNS MS OMENS oe a cis vacea cases ceovelen PlVitgeemer wane .ne: S.W. Australia 331
elevata. Pl. xvii. f. 63, 64,
TAL, SAT TE) Ree eee a
3
ceo Pl xvi, f. 72 ooik oc. .0s
symmetrica. Pl. xviii. f. 83...
violacea. Pl. xv. f. 26, Pl. xvii.
yarraensis. Pl. xv. f. 27, 28...
Mucronella duplicata. P\. xvi. f. 54
Clemanseme llevar. f. 91s oo 2...
mucronata. Pl. xvii. f. 66 ...
Porella denticulata. Pl. xvii. f. 70..
emendata. Pl. xvii. f. 69......
Porina clypeata. Pl. xvii. f. 67 ...
columnata. PI. xviii. f. 88 ... |
cGononatas “RI xv.t. 97 ..L... |
Retepora marsupiata. Pl. xv. f. 34—
36, Pl. xvii. f. 59, 61, 76, 77
|
|
|
|
| 332
|
|
|
\
rimata. P\. xvi. f. 48, 53...... 343
Schizoporella amphora ............4+ 341
australis. Pl. xiv. f.15. ...... | 341
conservata. Pl. xviii. f. 81 ... 340
— excubans. Pl. xvi. f. 56, Pl.
PMO! Eos) ow eisicecy iocave chess 341
PMCSEGRLOR Seth S. es oh xtostanwee. ) 339
Name of Species. |
FOSSILS FIGURED AND DESCRIBED.
Formation. Locality.
PoLyzoa (continued).
Schizoporella phymatopora. Pl. xv. \
[ERO IMBY-) Sham be a remeninsarsr re cen Hors |
spiroporina
submersa.
ventricosa
vigilans.
, Sp.
Selenaria alata
marginata.
Smittia anceps.
centralis
Peeters eeesetesecsese
CeCe ere ereeesereese esses
secrcceee
Pees ercereoesesssesesscoesesserecr
Ceo eoeee sere eres secees
Pixie!
Pl. xviii. f. 94
Cece eereSoescrsenes seessseae
BUGS)
Cech eereceesc ese sseesceseegsorr oe
Pl. xvii. f. 65
Stomatopora dissimilis
inflata
eoeoeecee
eertesroecesoccseeesoeecs cece
‘Miocene
S.W. Australia
oe I
Silurian
Silurian
eoceecocees| BILIUGAILILI w.cccvcces
Mo.uuusca.
(Lamellibranchiata.)
Trigonia densinoda
seoneseescseesessccae
|Purbeck
Dorsetshire ...
( Cephalopoda.)
Amaltheus subspinatus ......0....004.
Ammonites Braikenridgii
—— Brongniarti
cadomensis
concavus
Gervillii
—- Humphriesianus
linguiferus
— Mansel
eceveeserecsessesozsece
eoceec® 08 Cesseoe
eoceesseessscessss ene see
eeceocesetoseocc cee ess cs eee
Sececc SO Oeeeseeses seeceosecce
@eeeeersccescereecosesossssecsece
Subraditatusim--eencoscceneceteere
Cosmoceras Caumontii
Garantianum
ParkimsOMlsnn.ccuscee reece Cees
SOURED So5coabaccasoscocaoce
Haploceras oolithicum
Harpoceras adicrum
concayum
CONUS Cee s Pena
— cycloides
dispalisuimienennsesccsease cece:
— Edouardianum
—— fissilobatum ...............00-00-
evesquellyasr sj. Seki eaccine dese
Moorei
Murchisone ......... ane Ne aeane )
@eececsccsccses
e@oeeaeccesssece
eons ectcoceesecsrce
Coeee eo ee OOP eeoevesseses
|
> ball
Inferior Oolite...| Dorsetshire ... +
|
\
| Page.
338
340
340
338
338
339
345
344
337
337
337
337
615
615
| 246
FOSSILS FIGURED AND DESCRIBED. Xl
Name of Species. Formation. Locality. Page.
Motuvsca (continued).
( Cephalopoda, continued).
Harpoceras Sowerbyi...............-+. Nei (; 602
EYLOCCTUS CONFUSUIM .....00005..00000: | | | 601
——— Budesianum ...........:.-.ses00e 601
REPRE SUIS aw ores caicie-is\sie se oer «a | || 601
Oppelia subcostata ......... Re ercniades '! 607
SPUD ACUI AAS etter o/s wie oh tive sae bos 606
PRR U ET ea eres = ctclaic cia ciciaicis'o eer ee | 606
Perisphimctes Martinsii ............... 602
BV SIESUIN ose se cca caceee ese | 602
Spheroceras Brongniarti ............ 097
———— GEMOEPNUM « ...--.2.22-20+eseeee | 598
Mansel 02022070, F imferior Ootte....- Dorsetshire ...4 | 597
REMI CMS 80 ce ccioosciciini<seles once: 597
PoOlyMOTPHUM .2.2...52.....500- | 598
RMAC eaten sacs fe sic oi's'alvinlon 034s 196
IAL Dee c cies ou oor eiccie ns ocwe en 599
Stephanoceras Blagdeni............... | 595
RRC ONTIG SU). 20... ccc. ccecees ese 1 | 895
Deslongchampsii ............00. 595
— Humphriesianum ............... | 594
Hineaiferm, 82.3. ...6..2.c0ees ee | | 596
OUVAME TUT caer sci. sxle Saisie 2 ices | 596
OPO eee see sarees cwess a aeesles ) {| 596
VERTEBRATA.
(Pisces.)
Anodontacanthus acutus. PI). xxii. \ |
EUR ees sobdiicanciide ccesteeseo- | fe 428
spies. De sale ‘Coal-measures...) Yorkshire...... 498
Gurusise ble xxi to 1 2.25%: 428
Cladodus curtus. Pl. xxii. f.9 ...... \ (| 424
Ctenoptychius Ordii. Pl. xxii. f. 8. | | 422
PE CUUDANUIS Hence sc ccs scents oct tes | 424
Hybodus austiensis. Pl. xxii. f.1... | | | 416
pumetatus. Pl xxi. f.2-...... )|Rheetic.......c.-.: Bristol) 2.07.00. Slit Wf
Nemacanthus minor. Pl. xxii. f.5. | | 419
Paleosaurus Stricklandi. Pl. xxii. | 420
SPROMPPRRO Ere cco cede ces cess vaste |
Sphenonchus obtusus. PI. xxii. f. 7 ) \| 420
( Reptilia.)
; : re
ae Sos FL ae Cretaceous ...... | Folkestone ... 634
Adriosaurus Suessii. Pl. iv........ sei -NEOCOMMNanNn-ee-- | Comén,Trieste 55
viluxosaurus felinus.- Pl.ix. ...... |KarroO.........s0« South Africa.. 261
AGLOSAUTUS OTOCUIS ..0..cc00ss.0n see \ (| 700
Crateomus lepidophorus. P|. xxvii. | |
foo Pl xxvii. t.9; Pl xxix. \|Cretaceous .....-| Austria......... 4
foo. blo xxx. f. 2,5; Pl. xxxi. | |
Lé-5 ,.d er i (| 660
xii FOSSILS FIGURED AND DESCRIBED.
Name of Species.
Formation.
VERTEBRATA (continued).
(Reptilia, continued).
Crateomus Pawlowitschii. Pl. xxvii. \
f. 20; Pl. xxviii. f. 2-4; PI. XXIX.
1 Zh BB Pls 18 Gi, 455 lel 20:0.4l.
sp. Pl. xxvii.f.9-16 .......--
Crocodilus proavus. Pl. xxvii. f. 24-
26 sPle xxvinits OS) eel exis
f. 7-13; Pl. xxx. f. 6-14 .........
Doratodon carcharidens.......-++++++-
Emys Neumayri. Pi. xxvii. f. 273 |
Pixxx 6s, Plbsexxtstelioncse ("
Hoplosaurus ischyrus. Pl. xxx. |»
Dich ascliasnesicsaishs ac menmotrancsctstes
Megalosaurus pannoniensis. P). xxvii.
£223 reese once soeeee css:
Mochlodon Suessii. P1. xxvii. f. 1.. |
Ohigosaunustadelust penser reece
Ornithocheirus Bunzeli ..............-
Ornithomerus gracilis. Pl. xxviii. |
POs sseet aoslecteos Oameee ceaae y)
Platypodosaurus robustus. PIl.x....
Plesiosaurus brachycephalus. PI. \
D:D IN IY linen Nopenana) aon coddo stone |
Conybeart. PI. xxiil., Pl. xxiv. }
Cote ert cce ere ees ee eee COS Fees eroeceee
megacephalusaseeneeeteeeeeen eee )
Pleuropeltus Suessiz, Pl. xxviii. f. 8, \
Os PS xoxixe of 0165 3 ea ee etree a |
Rhadinosaurus alecimus. Pl. xxxi. |
EG NO 3 eee cadence tae eee r
Struthiosaurus austriacus. Pl. xxvii. |
56 em ee
’
(Mammalia.)
Balenoptera Juddi.........cccccececeee Oligocene
Ariconodonemordaxt esses. see Purbeck 2-2
Cretaceous
Cretaceous
eecoeeeos
Locality.
Austriaeee eres
South Africa..
Dorset
Hampshire ...
Dorset
eeecccee
~~ SS - SF
Page.
EXPLANATION OF THE PLATES.
PLATE PAGE
I. ) Microscoric Sections or Grits, and GraArns or Sanp, to il-
100 instrates Mire dean milli pss paper ea secteessss-eeee sek ee = 6
i Maps, Plans, and Sections of InrerauactAnL Deposits oF
Til West OCumMBERLAND AND Nortu LANCASHIRE, to illustrate
Mie ey Wendallignpaper vannciensuiaecesnesesrecsssesce «ses acts. 29
IV. f ApriosauRuS Sugssti, to illustrate Prof. Seeley’s paper on
TL Gust TR ecb ae SO A eee 52
SECTION OF THE CLIFFS IN ToTLAND AND CoLWELL Bays,
v Iste or Wicut, to illustrate the paper by Messrs. Keep-
mene t Cl Meh we MCI eee esac seta iapisicjotie wsiaielaclan “ccianisteeideeiisiansise.«s 85
VI SwepisH Cretaceous Crinoips, to illustrate Mr. P. H.
Wan Penber spa Peli eee ssc een ess ee caaceoecsc- Sens steoasae 128
yy, { Weusn, Crapornora, to illustrate Mr. C. Lapworth’s ap-
; pendix-to Mr: Walter Keeping’s paper .::.-..0.:--+..------0-- Wal
VIII “Map anv Secrions or ANGLESEY, to illustrate Dr. Calla-
‘ { WW LVES [DL CLAN sctueetccctoeeateia Mama nisme'sisl oleltccia-iale/sisiisiniciaaiierse ssitslesaicioe 210
1x, J Hvvrosavrvs rerinvs, to illustrate Prof. Owen's paper on
Elberta pbtlor mc racamemtesss sodeeaticenceesceteac aot sans suena toes 2
x, { Puarypoposaurus RoBustus, to illustrate Prof. Owen’s paper
Gin, WANG TSO hes waaneBa ston ynan dakke Lacea saeO Bec DRARUECE nem eoneaee 266
XI Map sHowING THE Rocks OF THE CARLISLE Basin, to illustrate
Mir eV eOlmeaiskpaner., a taenne ates tae sete seo. wesaee. 286
Sate | Drvonran Prants, to illustrate Dr. J. W. Dawson’s paper... 299
XIV. \
ae | Victorian Fossint Bryozoa, to illustrate Mr. A. W. Waters’s
XVII. | } 02) 02 SSS SoS COCO OBOOS OOS SO COO COCOOO Sc OOOO COCOUC KOO GeOSoUOUnCOnOSOomon: 309
XVIIL )
X1V EXPLANATION OF PLATES.
PLATE PAGE
JuRAssic DriAstoporrps, to illustrate Mr. G. R. Vine’s
XLEXG
DAPOL" seis ages ouacaninnk Getinamas eaten neice ean an eaeena cece ee eeenee 381
Xx Microscoric Sections or Virreous Rocks or Montana, to
illustrate; Marsh Roubley(s) papers... accent hee eeeeeeee 391
XXI Microscoric Structure or WetsH LAVAS or Low&r SILURIAN
ae Agu, to illustrate: Mir. Ee Rutleys paper) 2. ...s-4-e4-eeeeeees 403
XXII FHISH-REMAINS FROM THE Aust BoNE-BED AND THE COAL-
MEASURES, to illustrate Mr. J. W. Davis's papers ...... 414,427
XXIII. ) Puestosaurus ConyBEARI AND P. BRACHYCEPHALUS, to illustrate
XXIV Prof. W. J. Sollas’s paper on those reptiles .................. 440
XXV. Sinurtan Piant-remarns, to illustrate Dr. Hicks’s paper ... 482
ComPARATIVE Sections or Upper JURASSIC Rocks In FRANCE
XXVI. | AND EnGuanD, to illustrate Prof. Blake’s paper ............... 497
OTE \
VIII.
XXVIII. | REMAINS oF REPTILIA FROM THE GosAu ForMATION AT WIENER
a f Nevsrant, to illustrate Prof. Seeley’s paper.................. 620
OO)
ERRATA ET CORRIGENDA.
Page 197, line 12 from bottom. for these read there.
Pages 305 and 307, line 10 from bottom for Peny read Perry.
Page 306, line 15 for Bodun read Brown.
Page 307, line 30 for magnacensis read gaspiensis, and delete footnote.
Page 326, line 15 from bottom, for DENTIPOR read DENTIPORA.
Page 406, explanation of Fig. 1, for Fisst/e read Felsite.
Page 597, line 3 from bottom, for Mansrniui read MANSELII.
Page 597, line 2 from bottom, for Mansellii read Manseliv.
THE
QUARTERLY JOURNAL
OF
THE GEOLOGICAL SOCIETY OF LONDON.
Vou. XXXVII.
‘1. Nore on the Occurrence of Remarns of Recent Pants in
Brown Iron-orzr. By J. Anruur Purtiirs, Esq., F.GS.
(Read November 3, 1880.)
Tuts bed of fossiliferous iron-ore is situated at Rio Tinto, in the
province of Huelva, Spain, and is in close proximity to the cele-
brated copper-mines of that name.
In this portion of Southern Spain deposits of cupreous iron
pyrites, consisting of a series of lenticular masses of ore, having a
general direction a little north of east and south of west, extend
from Aznalcollar, near Seville, in the east, for a distance of more
than seventy miles westward to within the Portuguese frontier.
At Rio Tinto the deposits of this mineral are very extensive, and
consist of a compact and intimate admixture of iron pyrites with a
little copper pyrites, through which strings of the latter mineral
- sometimes ramify.
Although these mines appear to have been worked, and the copper
smelted upon the spot, from time immemorial, it is evident from the
vast heaps of furnace-slags, and from the extent of the various other
remains in which coins and inscriptions of the reigns of the
Emperors from Nerva to Honorius have been discovered, that their
great development under the Romans took place during the first four
centuries of the Christian era. After the fall of the Roman empire
they seem to have been abandoned down to as late as the year 1727,
from which date they were intermittently worked by the Spanish
Q.J.G.8. No. 145. B
2 J. A. PHILLIPS ON THE OCCURRENCE OF REMAINS
Government and by various private speculators until 1873, when
they were purchased by an English company. The extent of the
mining and metallurgical operations anciently carried on in this
district will be understood when it is stated that at Rio Tinto alone,
in addition to hundreds of Roman shafts and miles of Roman
galleries, the heaps of copper slags resulting from the smelting at
that period cannot amount to much less than one and a half million
of tons, and that there are large accumulations of similar ancient
refuse at Tharsis, Buitron, and omen mines.
As illustrating the care and skill of the metallurgists of that period
it may be stated that each ton of their slags seldom contains above
three pounds of copper.
The prevailing rock throughout this region is clay-slate, which,
from the evidence of various fossils found by Mr. A. Hill, Mr.
G. W. Clement, and other officers on the staff at Rio Tinto, is
apparently of Silurian age. These specimens were kindly examined
by Mr. R. Etheridge, who did not hesitate to identify them as
belonging to that period.
These slates are, in places, broken through by large dykes of
quartz-porphyry, which frequently form one of the walls of the
various deposits of cupreous pyrites.
The fossiliferous iron-ore which is the immediate subject of this
note forms a cap one kilometre long, with an average width of one
hundred and thirty metres, on the top of the Mésa de los Pinos,
nine hundred metres south of the open cutting at Rio Tinto. Its
surface is approximately level, but it varies m depth from one to
seventeen metres in accordance with the conformation of the surface
of the slate upon which it lies ; the rock beneath it is bleached and
to some extent decomposed.
The order and relative positions of the several formations will be
best understood on referring to the accompanying plan and section
(figs. 1, 2), for which I am indebted to Mr. Neil Kennedy, a gentile-
man in charge of a portion of the work at the mines, through whose
kindness I am also enabled to lay specimens of the fossiliferous iron-
ore upon the table.
On the extreme right of the section is a broad porphyritic dyke
forming the north wall of the south lode, next to which is the lode
itself, which at this point has only one third of its greatest width.
iNest in succession, to the south, comes a band of slate, which
is again penetrated on the left by a broad dyke of quartz-porphyry.
tt will be observed that the upper part of the vein has, to. a con-
siderable depth, been converted into a ferruginous capping (gossan),
of which a large portion has been removed by denudation. The
stratum of iron-ore forming the surface at the Mésa de los Pinos
is shown with precipitous sides; and a small patch of a similar
formation occurs, at within a metre of the same elevation, at the
Cerro de las Vacas. Numerous fissures occur in the surface of the,
larger deposit of iron-ore, and out of these pine-trees formerly
grew in considerable numbers, their presence giving the name to
the locality ; these were eventually destroyed by sulphurous fumes
OF RECENT PLANTS IN BROWN IRON-ORE. 3
Fig. 1.— Plan of part of Rio Tinto.
SY
i ope SA L/w
ee ay ROWE
Y Ws
MWg Cory, iy ae ,, = —. Ce TTOS¢ loan —
Phe (E Z LUN
. ) INEZ
a ed
: 1
Seale of Plan and Section 15,000
Fig. 2.—Section in line AB on Plan.
p.W N.E.
South Mésa de Rio Cerro de South Cerro
Dam. los Pinos. Agrio. las Vacas. Lode. Salomon.
ee
‘
{
1
1
1
1
i
1
t
aA Mian Ah) Ten YN OPEN DO
Th I] i) “ TMM HH] ISO
SUIS Hi HUH i lh HH MEMS MA) SESSEAIS S/R AEN
See)
7:'| Capping of lode.
Mineral.
resulting from the metallurgical operations which were carried on
upon the declivity of the opposite hill.
In some instances the decomposed clay-slate has been partially
removed from beneath the iron-ore, from which blocks have been
detached, and have slidden a considerable distance down the surface
of the slaty declivity.
A specimen of this iron-ore, analy a in my laboratory, afforded
the following results :—
BQ
4 J. A, PHILLIPS ON THE OCCURRENCE OF REMAINS
(Ghivesromlebnic me iar ieee 1:40
Wis | Ree RO SAIa Tren 11°85
ISU CAF Baro anno ei oo bod 6:5 1:53
MerniCloxide ies. ener wm iw 84°65
AU TAaMAT TG 3, coe eueoraye cs puede eset ee trace.
Phosphoric anhydrides - 4. -4e)e- 14
PiU 0) COU Ree AA anc ACA as cach ene 23
99°80
It follows that this is a rich ore of iron of fairly good quality ; and
as there is now a well-appointed railway in its immediate proximity,
it is probable that under moderately favourable conditions of the
iron trade it may be worked with advantage.
During the process of quarrying this ironstone for exportation,
Mr. Kennedy first observed the presence of fossil remains of what
appeared to be leaves and seeds of many of the plants still growing
in the neighbourhood, as well as of several well-preserved beetles.
All doubt as regards the recent character of these fossils is, how-
ever, removed by the following communication from Mr. W. Carruthers,
who kindly undertook their examination, and who says, “‘ The speci-
mens you have sent me for examination from Rio Tinto contain the
following fragments of plants which I have been able to identify :—
leaves and acorns of Quercus Ilex, Linn.; leaves and seed of a two-
leaved species of Pinus, most probably Pinus Pinea, Linn.; the cone
of Equsetum arvense, Linn.; and a small branch of a species of Erica.
There is also a well-marked leaf of a Dicotyledonous plant which
I have not yet been able to identify. The greater portion of two of
the specimens consists of a thick growth of moss, but it is impossible
to say what the species are. ‘The whole is permeated with minute
branching roots, showing that the vegetation was formed as a peat-
moss, the oak- and pine-leaves being carried or blown into it. The
plants are evidently, all of them, the same species as are still found
growing in Spain.”
In addition to these fossils this deposit sometimes aorta minute
concretionary patches of imperfectly crystallized quartz.
Every one who examines the section extending from the Cerro
Salomon across the valley of the Rio Agrio to the Mésa de los
Pinos will probably agree that the origin of this deposit of iron-ore
can scarcely be doubtful. At the time of its formation a marsh or
shallow lake extended from beyond the last-named point to the foot
of Salomon, and into this flowed solutions of iron-salts resulting
from the decomposition of the upper portions of the immense masses
of pyrites constituting the south lode.
From these salts oxide of iron was deposited, as in the case of
bog iron-ores generally ; and, finally, the valley of the Rio Agrio was
eroded, as well as that south of the deposit, leaving the Mésa
capped with iron-ore, while a small patch of the same mineral
was left at the Cerro de las Vacas.
That the deposit took place at a comparatively recent date is
evident from the fossils it contains; and it is equally certain that the
OF RECENT PLANTS IN BROWN IRON-ORE. 5
erosion of the valley is older than the occupation of the district by
the Romans. Not only are numerous remains of buildings and other
works belonging to the Roman period found in the valleys, but the
Roman grave-stones, of which scores are still scattered over some
parts of the district, are invariably made of this iron-ore.
Discussion,
Mr. CarrurHers pointed out that the deposit, though of such
thickness and importance, was essentially a bog iron-ore and, like
ores of that character, contained remains of recent plants.
The Prestpent remarked on the difference in appearance of mas-
sive hematites from ordinary bog iron-ores and those brought by the
author of the paper.
Dr. Sorsy asked if it were possible that these could have been
deposits produced by springs, such as occur on the hill-sides of
Yorkshire, and are still forming.
Mr. Parrison stated that the bog-ore deposits in Ireland occur
on the sides and summits of hills, and that the Rio-Tinto deposit is
a true bog iron-ore.
Mr. Bavprman remarked on the resemblance between this ore
and that of Arklow, which is also derived from pyrites ; and con-
sidered that the freedom from phosphorus was to be attributed to
their rapid and direct formation as compared with ordinary bog
iron-ore, which is contaminated by accessory products of decompo-
sition from organisms and rock-masses.
The AvutHor, in reply to Dr. Sorby, stated that the top of the
deposit was regular and the bottom irregular, leading to the belief
that it was probably a deposit in water. Further he indicated that
there is an outlier on the same level. The hard cap is sometimes
undercut by denudation. He remarked that springs are scarce over
the whole district, and that there are none containing more than
traces of iron in solution.
6 J. A. PHILLIPS ON THE CONSTITUTION AND
2. On the Constitution and History of Grits and SanpstonEs. By
J. Antour Puittres, Esq., F.G.8. (Read December 15, 1880.)
[Puares I. & IT]
Te careful and exhaustive researches relative to the constitution
and mode of formation of arenaceous rocks which have recently been
published by Professor Daubrée, Dr. Sorby, and others, leave open a
comparatively restricted field for the pursuit of similar investiga-
tions. Having, however, during the last two years paid considerable
attention to the study of rocks of this class, I now venture to bring
before the notice of the Geological Society some facts and deductions
- therefrom which would appear to have escaped the attention of
previous observers.
For the convenience of developing certain ideas relative to this
subject, I propose in the present paper, in the first place, to describe
various grits and sandstones which have been microscopically and
otherwise examined. In doing this the older rocks will be con-
sidered first, and those of more recent age subsequently noticed in
the order of their geological sequence. The chemical composition
of some typical rocks will also be given.
Secondly, the results of observations bearing on the effects pro-
duced by the action of flowing water on particles of sand and gravel
transported thereby will be described ; and finally, the more impor-
tant observed facts will be summarized,.and their bearings discussed.
The difference between grit and sandstone is one not always
distinctly marked ; and numerous definitions of the two rocks, often
somewhat contradictory, have been given by various geologists at
different times. It has even been stated by an eminent authority
that rocks which in the north of England would be called grits,
receive the name of sandstones in the south *,
In order, therefore, to avoid misunderstanding upon this point,
I may state that in the following descriptions the term grit is
applied only to coarse-grained arenaceous rocks of which the com-
ponent fragments are for the most part angular, and which, although
frequently crystalline in structure, seldom contain either perfect or
nearly perfect crystals. The cementing material of such rocks is,
as a rule, highly siliceous.
Sandstones differ from grits in being finer in ‘structure than the
latter, and in their component ¢ erains being usually less completely
incorporated with the cementing median The quartz in many
sandstones occurs principally in the form of perfect erystals, or in
that of crystalline aggregations.
In quartzites the spaces between the component grains are com-
pletely filled by a siliceous cement, in which respect they closely
resemble some varieties of fine-grained grit.
* “Manual of Geology,’ by John Phillips, F.RB.S., p. 654.
Quart. Journ.Geol. Soc Vol. XXXVII. P11.
imp.
Mimtrn Bros.
8
i
x
X78
del.
Frank Rutl ey,
vi CMON Ob GRIMS:
AN ee
vXV
\
V
S45 LN
a]
|
au
VO
J
inp
tern Bros.
ifie
Sel.
ey, a
_ Rat
say
Fra
2
van
an y
:
~ HISTORY OF GRITS AND SANDSTONES.
NI
Composition and Structure.
Cambrian.— The well-known Barmouth Grits of North Wales,
which occupy a large extent of country lying between Barmouth
and Harlech, are usually of a greenish-grey colour. They are ex-
tremely hard, and often enclose angular fragments of quartz above
a quarter of an inch in diameter. Sometimes these grits become
fine-grained, and assume a purple tint ; they are intermingled with
occasional bands of greyish-green and bluish slates, which, especially
towards the lower part of the series, attain considerable develop-
ment. Of these rocks Professor Ramsay remarks :—‘“ The beds seem
to have been formed principally by the direct waste of rocks of a
granitic character, or at least into the composition of which crystal-
line quartz and felspar largely enter ”*.
When a thin section of this rock is examined under the micro-
scope, it is seen to consist, mainly, of an aggregation of fragmentary
quartz and felspar united by a siliceous cement, which is throughout
permeated by a moss-like greenish mineral, a portion of which is
probably chlorite. ‘The larger pieces of quartz and feispar are often
distinctly rounded, although they also sometimes present irregular
and perfectly sharp outlines. Hig. 1, Pl. 1I., drawn by Mr. F. Rutley,
represents, in black and white, a section of this rock as seen in
polarized light, magnified 18 diameters, and containing much felspar.
The quartz occasionally contains liquid-cavities enclosing moving
bubbles, but these are by no means numerous; the greenish mineral
of the cement sometimes penetrates into fissures 1n the siliceous
grains. ‘Two distinct species of felspar are present in considerable
quantities, the larger grains being, for the most part, somewhat
rounded fragments, which, after having assumed the form of
pebbles, have sometimes been broken across their smaller dia-
meter, thus presenting one angular and one rounded termination.
The orthoclase is not much altered; and a triclinic felspar, which,
from the optical properties it exhibits, is probably oligoclase, shows
brilliant lines of twinning when seen in polarized light. Some
of the quartz encloses hair-like crystals of rutile, while calcite,
magnetite, iron pyrites, and a few imperfect garnets are present in
the cementing siliceous base. An analysis of this rock is given,
page 21.
The grits in the neighbourhood of Harlech are usually finer in
grain than the foregoing, but otherwise differ from it only in con-
taining a few imperfect crystals of epidote.
Stlurvan.—Stiper Stone, from the neighbourhood of Shrewsbury, is
a fine-grained and exceedingly hard sandstone, the grains of which
are so closely cemented together by crystalline silica as to form a
quartzite. Many of the fragments of quartz, of which this rock
is mainly composed, are somewhat cloudy and are considerably
rounded, while others are colourless and transparent, with but few
fluid-cavities, which are, for the most part, full. The average dia-
meter of the grains is about +, inch, and some of the most pebble-
* Geology of North Wales, p. 17, ed. 1.
8 J. A. PHILLIPS ON THE CONSTITUTION AND
like among them form the nucleus of a crystalline growth of colour-
less transparent quartz, which converts them into more or less perfect
crystals of that mineral. Felspar is not abundant, and is often
considerably altered ; the cementing material occasionally contains
minute crystals of a mineral which is probably epidote.
A grit of a grey colour, speckled with minute white points, from
the neighbourhood of Aberystwith, is seen under the microscope to
be composed of an almost equal amount of quartzose and felspathic
grains united by a siliceous cement, everywhere permeated by a
moss-like chloritic mineral, to which reference has already been
made. In this rock the constituent fragments are sometimes as much
as = inch in length, and their angles are usually to a certain extent
rounded, although they occasionally exhibit very sharp and irregular
outlines. The quartz, which exceptionally contains a few needles
of schorl, is colourless and transparent, containing exceedingly
minute fluid-cavities, of which the majority are full, although others
enclose constantly moving bubbles.
The felspar has been subjected to considerable alteration, and is
not unfrequently obscured by flocculent microlths resulting from
chemical re-combinations ; a portion of it, however, evidently belongs
to a triclinic species. In addition to the above, there are inclusions
which are undoubtedly fragments of a volcanic rock of basaltic
character.
The siliceous cement contains a few crystals of iron pyrites, as
well as small flakes of brown and colourless mica, of which the
edges are much rounded.
It is evident that some portion, at least, of the quartz constituting
this grit has been derived from the disintegration of quartz-felsite
(quartz-porphyry), since its general characteristics are not only
similar, but it, moreover, includes the blebby masses of an ater ee
ground-mass SO characteristic of the quartz of such rocks.
A fine-grained foliated rock belonging to the same series, from
ae ae Botmetmnes locally called a grit, of which the grains
vary from <4, to zgbp inch in diameter, has a composition gene-
rally similar to that of the foregoing. In addition, however, it con-
tains numerous water-worn flakes of mica, which occur chiefly in
distinct bands, and which are arranged with their cleavage-surfaces
parallel to the plane of foliation of the rock. The fragments of
quartz, which are of a nearly uniform size, are all sharply angular,
and elongated or flattened grains are rare.
An examination of sections prepared from May-Hill Sandstone,
containing numerous casts of Pentamerus oblongqus, aoe that this
rock is mainly composed of angular grains about z00 inch in dia-
meter, united by a turbid siliceous cement, suggesting the idea of
its “haraime been deposited from waters holding clay in suspension.
In addition to the smaller grains, of nearly equal dimensions, there
are a few fragments of, at least, four times the size above stated.
These, like the smaller ones, sometimes contain a few hair-like
crystals of rutile; but fluid-cayities containing bubbles are exceed-
ingly rare.
HISTORY OF GRITS AND SANDSTONES. 9
Sandstones, or rather quartzites, of Upper-Llandovery age are
developed in the Lower Lickey hills in Worcestershire. A specimen
from this locality was found to be chiefly composed of much-rounded
grains of quartz, having an average diameter of = inch, cemented
together by a growth of transparent crystalline quartz. "This mode
of | formation is rendered evident by the circumstance of the rounded
grains being frequently composed of cloudy or slightly turbid quartz,
while the cementing silica is perfectly colourless and transparent.
When examined in polarized light, the cementing quartz is seen to
exhibit, fora certain distance around each grain, the same colour as
the grain itself, and appears to have been deposited in crystalline
continuity therewith. Fluid-cavities, with bubbles, are numerous in
some of the grains, while others are entirely without them. Rutile
and schorl are sometimes present in the form of minute crystals.
A specimen of Denbighshire grit from Pont Cletwr Yspytty,
when examined, was found to consist of an exceedingly fine-grained
mosaic of cementing concrete containing minute granules of quartz,
and enclosing larger fragments of the same miner fle with Hel sien and
colourless or brown mica, each grain being from = to >j> inch in
diameter. Some of the quartz fragments are so traversed by the
moss-like greenish mineral, often forming a constituent of the cement
of sandstones, as almost to suggest the idea of their being pseudo-
morphs after a mineral which has disappeared. If seen in polarized
light, however, they will be observed to be each made up of several
distinct grains, in the fissures between which the substance referred
to has obviously been deposited. The quartz of this sandstone occa-
sionally encloses a few needles of schorl or hair-like crystals of
rutile ; cavities containing bubbles are rare.
A rock belonging to the Coniston-Grit series from Green-quarter
Feli, Westmoreland, consists of angular grains of quartz and felspar,
united by a siliceous cement traversed in all directions by numerous
greenish BEerouths. The average size of its constituent particles
does not exceed 5,45 inch, allow there are a few larger ones,
measur.ng about 1, inch in came cen! The quartz contains on fluid-
- cavities with bubbles ; but when these occur they are extremely
minute. This rock contains a little iron pyrites, and the cement is
sometimes stained by hydrated ferric oxide; a few flakes of colour-
less and dark-brown mica are occasionally seen between the grains
of quartz and felspar.
Devonian.—The majority of the siliceous grits of Cornwall are
usually regarded as being of Devonian age; but it is probable that
some of them may be of older date.
-Two distinct beds of such rock, of a greenish-grey colour, which
are worked for road-metal, are quarried on the farms of Tregian and
Dairy, in the parish of St. Ewe, near St. Austell, and were noticed
in a previous paper under the name of slaty agglomerates*.
In both these localities the grit contains angular fragments of a
soft clay-slate of a greenish-blue colour, and is exceedingly hard
and tough. The rock quarried at Tregian is composed of a mixture
* Quart. Journ. Geol. Soc. 1878, vol. xxxiv. p. 476.
10 J. A. PHILLIPS ON THE CONSTITUTION AND
of angular pieces of quartz and felspar, of which some of the
larger fragments have a diameter of =, inch; they are cemented by
a siliceous concrete enclosing particles of granular quartz, through
which minute greenish microliths are plentifully disseminated.
Comparatively few fluid-cavities, either with or without bubbles,
are present. In addition this rock contains a few crystals of schorl
enclosed in the quartz, some water-worn flakes of silvery-white
mica, a few crystals of pyrites, and perhaps a little altered mag-
netite. The felspar chiefly belongs to a triclinic species, but ortho-
clase is also present. The rock at Dairy differs from that at Tregian
only inasmuch as it contains a few water-worn crystals of horn-
blende and a little magnetite.
In addition to the foregoing, through the kindness of Mr. J. H.
Collins, I have been enabled to examine four other specimens of
Cornish grit, namely, one from St. Allen, four miles north of Truro,
two from Ladock, five miles further east, and one from Perranzabuloe,
on the Bristol Channel.
Hand specimens of all these rocks closely resemble one another,
excepting that those from Ladock enclose numerous angular frag-
ments of a greenish slate, which the others do not, and that one of
them contains a number of rounded quartzose and other grains 7 inch
in diameter.
When examined under the microscope, the St. Allen grit differs
little from those at St. Ewe; the quartz is angular and transparent,
the largest fragments having a diameter of about = inch, and they
sometimes, though rarely, enclose minute crystals of tourmaline. A
little hornblende, with white mica and epidote, are also present.
The felspar is, to a large extent, triclinic, but there is also some
altered orthoclase ; the quartz contains but few fluid-cavities.
In the rock from Ladock, which contains small rounded grains of
quartz, felspar, and other material, these bodies are sparsely dissemi-
nated throughout the mass of the normal grit; and a microscopical
examination shows that some of them are fragments of volcanic
rocks closely akin to the “‘ greenstones” and “ dunstones” of many
parts of Cornwall, but which have often become so altered as to be
recognizable only by their felspars and general structure.
Fig. 2, Pl. I., represents, in black and white, a fragment of volcanic
rock which occurs in this grit, as seen in polarized light, magnified
18 diameters.
The second specimen from this district is made up chiefly of angular
fragments of quartz and felspar, united by the usual cementing con-
crete. It contains a considerable amount of felspar, a large propor-
tion of which is triclinic. The largest pieces of quartz are about
;'z inch in diameter ; and fluid-cavities, although by no means abun-
dant, are more plentiful than they are in the Cornish grits before
described. Some of the quartz contains a notable quantity of dis-
seminated epidote (?), and flakes of white mica are frequently jammed
between the fragments of which the rock iscomposed. A few minute
garnets are present, as well as some fragments of a volcanic rock.
The microscopical structure of the gritty rock from Perranzabuloe so
closely resembles that of those from the other localities that a special
HISTORY OF GRITS AND SANDSTONES. J1
description of it is unnecessary. The felspar, of which a large pro-
portion is triclinic, is present in large quantities; and, as in the
case of the other specimens examined, the quartz contains but few
fluid-cavities. It will be observed that in this respect the quartz of
these grits materially differs from that of the Cornish granites, in
which fluid-cavities with bubbles are abundant.
Carboniferous.—A. fine-grained yellowish-white sandstone from
Shalk Beck, Cumberland, belonging to the Yoredale series, much
spotted by stains of hydrated ferric oxide, and rendered somewhat
mealy a) the presence of kaolin, contains but few fragments of more
than ;4, ich in diameter. The quartz is in angular pieces, colour-
less and transparent, and, to a large extent, free from fluid-cavities,
which, when present, are, for the most part, full, and consequently
without bubbles. In addition to quartz, with a little felspar and
kaolin, the only recognizable mineral is white mica. For the
analysis, see p. 21.
A sandstone from Brigham, Cumberland, belonging to the Mill-
stone-Grit series, was examined both microscopically and chemically,
and is essentially composed of a of quartz with a little fel-
spar, the grains being usually about +45 inch in diameter, united by
a siliceous cement, which j is sometimes a little cloudy. Between the
- constituent fraements of this rock there are sometimes minute
erystals of a mineral which may perhaps be epidote; and the quartz,
which is colourless and transparent, encloses a few needles of tour-
maline, besides containing occasional fluid-cavities, but few of which
contain bubbles. For the chemical composition of this sandstone,
see page 21.
AtSpinkwell quarry, near Bradford, a foliated siliceous sandstone,
which can be raised in the form of very large slabs, is worked in the
Lower Coal-measures, and is much used in the construction of chemical
apparatus on a manufacturing scale. This sandstone is mainly com-
posed of fragmentary quartz and felspar, of the latter of which a
portion is triclinic, united by the usual siliceous cement. The
quartz is colourless and transparent, and contains but few fluid-
cavities, although it sometimes encloses needles of schorl.
In addition to quartz and felspar, this rock contains kaolin, with a
few minute garnets, and flakes of dark-brown and colourless mica,
which are more abundant along certain lines of foliation than else-
where. A few minute crystalline scales of micaceous oxide of iron
were observed in the eas of this sandstone. The component
fragments rarely exceed 51, inch in diameter. For analysis of this
rock, see page 21.
The fine-grained yellowish-grey Coal-measure sandstone of Stony-
hough, Workington, Cumberland, is, to a large extent, oe of
minute crystals. or crystalline ageregations oi quartz of about 51,
inch in diameter, somewhat loosely united by a siliceous cement,
often much stained by hydrated ferric oxide.
A considerable number of sandstones belonging to the Carboni-
ferous period are chiefly composed of quartz crystals, which have
evidently crystallized in situ, since they exhibit the freshness of out-
line peculiar to crystals which have not been subjected to the slightest
1s J. A. PHILLIPS ON THE CONSTITUTION AND
amount of abrasion subsequently to their formation, not a point being
broken or an angle removed. Sometimes the original grains of
quartz have, by the subsequent deposit of silica upon their surfaces,
become converted into complete double-terminated crystals; but
the forms are frequently less simple, and the faces bounding the ex-
terior cannot all be referred tothe same crystal. That this crystal-
lization is produced by a deposit of silica around the original grains
of quartz, subsequently to their having become members of an accu-
mulation of sand, was first noticed in British rocks by Professor
Bonney*, and has been subsequently demonstrated by Dr. Sorby 7.
It is almost equally certain, as will be subsequently shown, that a
portion, at least, of the silica so deposited has been derived from the
decomposition of felspar.
Among highly crystalline Carboniferous sandstones may be men-
tioned one belonging to the Mountain-Limestone series, which occurs
at Yeathouse, in Cumberland, that of Parkhead, in the same county,
and that of Augill, near Brough, Westmoreland; the two last of
Yoredale age. Another sandstone in the Lower Coal-measures,
worked at Barngill quarry, in the county of Cumberland, is also
crystalline.
Permian.—The St. Bees Sandstone, at Rheda, Cumberland, is a
fine-grained reddish-brown rock, composed of a mixture of angular -
fragments and minute crystals of quartz with a little felspar, the
whole being united by a cement rendered, to some extent, opaque
by ferric hydrate. The grains and crystals of quartz have usually a
diameter of about 54, inch, and contain but few fluid-cavities. The
colour of this sandstone, like that of the majority of similar rocks, is
caused by a coating of hydrated oxide of iron over the surfaces of
the grains and crystals of which it is composed, but which is readily
removed by digestion in acids. Felspar is present in notable quan-
tity, and is often considerably altered; no triclinic species was
observed. A small amount of colourless mica is present in the form
of water-worn flakes, together with a few imperfect crystals of
schorl.
Numerous other crystalline sandstones of Permian age might be
cited; but those of Penrith, which have been described by Dr. Sorby,
are probably the most interesting and remarkable examples.
Triassic.—Among the Bunter sandstones of Lancashire and Che-
shire are certain reddish-brown friable beds, possessing but little
cohesion, and of which the constituent grains are all so completely
rounded, that the disintegrated sand flows between the fingers as
readily as shot. Deposits of such sandstones, which are distin-
guished by the name of “ Millet-seed beds,” occur plentifully in
the Lower Mottled series, and occasionally among the Upper Mottled
sandstones, as well as in the Frodsham beds of the Keuper.
A specimen of millet-seed sandstone from the Lower Bunter,
obtained in the form of a core, at a depth of 1039 feet, from the
* Quart. Journ. Geol. Soc. vol. xxxy. p. 666.
+ Address delivered at Anniversary Meeting of the Geological Society of
London, 20th February, 1880, p. 36.
HISTORY OF GRITS AND SANDSTONES. 13
Bootle bore-hole of the Liverpool water-works, was, with a large
number of others from that district, kindly furnished to me by Mr.
Charles HE. De Rance, of the Geological Survey, but was found to
be too friable to admit of the preparation from it of thin sections.
On examination by reflected ght, however, it was found to be so
entirely made up of rounded grains, varying in diameter from +,
to st, of an inch, that I did not hesitate to suggest to Mr. De
Rance the probability of its origin being due to blown sands united
by a ferruginous cement.
These grains, of which the majority are quartz, are so rounded as
to represent miniature pebbles, while a few, consisting of partially
decomposed felspar, are often corroded into deep cavities on one or
more of their sides.
The granules of quartz, as well as those of felspar, have been
covered by a thin coating of hydrated ferric oxide; while on the
surfaces of the former a beautiful growth of crystals of trans-
parent quartz has frequently taken place.
These crystals do not often exceed +4, inch in length; but they are
sometimes very perfect, with sharply defined angles, and frequently
exhibit both plagihedral modifications and horizontal striation. A
few crystals of pyrites and of calcite have also been formed on the
surfaces of the rounded quartz-grains.
Figs. 1, 2, 3, and 5, Pl. Il., drawn by Mr. F. Rutley from
specimens which I selected for that purpose, and magnified one
hundred diameters, represent crystals of quartz attached to rounded
grains of the same mineral forming the basis of this sandstone.
Fig. 4, magnified to the same extent as the others, is a grain of
quartz which exhibits a depression at its point of contact with
another similar body. Specimens presenting this appearance, which
are not very numerous, may sometimes be the result of one grain of
quartz having been forced or ground into the substance of another.
A careful examination, however, of such depressions leads to the
conclusion that in some cases when this pitting of a grain is ob-
served a deposit of silica may have taken place upon all parts of its
_ surface, excepting where it has been protected by contact with
adjoining grains.
Angular cores of a siliceous material which have been deposited
in cavities at the point of junction of several grains are sometimes
detached when the rock is carefully disintegrated by friction with
a hard brush. When these adhere to one only of the adjacent
grains, haying separated from the others, they obviously might give
rise to depressions of the kind referred to.
If, after treating this sandstone by hydrochloric acid, the residue
be examined under the microscope, the presence of these siliceous
bodies becomes at once apparent. They are sometimes slightly
coloured by ferric oxide, and do not always exhibit colours when
seen in polarized light; in other cases they afford evidence of im-
perfect crystalline structure, and are occasionally colourless and
transparent.
Fig. 6, Pl. II., is a grain of felspar which has become so corroded
14 J. A. PHILLIPS ON THE CONSTITUTION AND
that two distinct cavities have been produced in its substance. A
erystal of iron pyrites attached to a rounded grain of quartz is seen
in fig. 7, which, as well as the preceding figure, is represented as
magnified to the same extent as the other illustrations contained in
the Plate.
Prolonged digestion in hydrochloric acid removes the oxide of
iron, leaving the surfaces of the rounded quartz granules clean
and colourless. The minute crystals of quartz which have been
formed upon them, however, adhere firmly to the rounded grains,
after this treatment, and no stain of ferruginous matter can be
observed between their point of attachment and the grain of sand
on which they have been formed. It would therefore appear
that, although the sand had been covered generally by ferric hy-
drates previous to the growth of quartz crystals, these have never-
theless originated at those points only where a chemically clean
surface of the quartzose nucleus was exposed. An analysis of this
sandstone is given, p. 21.
Sandstones chiefly composed of rounded weather-worn grains occur
in the Lower Mottled series, at a depth of 80 feet from the surface
at Stock’s Well, belonging to the Widnes water-works, and at
Scott’s bore-hole near St. Helens, as well as at a depth of 260 feet
in the Winwick boring of the Warrington water-works.
Beds of loose, rounded sand of the age of the Lower Mottled
Sandstone are known to occur at Chapel Bridge, Prescot, and in a
boring a little east of Newton Bridge, near Warrington.
Sandstones of this character are met with north of Eccleston hill,
and asimilar bed belonging to the Upper Mottled group comes to the
surface in the yard of the Bridgewater Foundry at Runcorn. By
no means, however, do all the sandstones of Lancashire and Cheshire
which belong to this geological age exhibit characteristics suggestive
of their formation from eolian sands. At Wirral, in Cheshire, as
well as sometimes in the neighbourhood of Liverpool, the Pebble-
beds of the Bunter are represented by a brownish-yellow sandstone
containing numerous pebbles, which is much employed for building-
purposes.
In many of these beds the quartz is almost entirely in the form of
minute crystals, or crystalline aggregations, often united by a ferru-
ginous cement, which has manifestly been introduced subsequently
to the covering of the original grains with crystalline quartz.
An excelient example of a non-ferruginous crystallized sandstone
belonging to the Upper Mottled group occurs at Town Green, near
Ormskirk. This rock is mainly composed of crystals of transparent
quartz, of which the edges and angles are beautifully perfect. It
is of a far too friable nature to allow of the preparation of thin
sections ; but it appears to have little or no cementing material, and
to be, to a large extent, merely felted together by the intergrowth
of its constituent crystals. It will be needless to remark that the
grains of sandstones of Bunter age are not always oleae rounded or
enveloped i in crystals of quartz.
Among the Keuper division of the Triassic candauinen which are
HISTORY OF GRITS AND SANDSTONES. 15
mainly composed of well-rounded siliceous grains, may be cited a
grey, friable, fine-grained rock from the base of this formation,
which is exposed in the railway-cutting at the Runcorn station,
and a dark-red sandstone of still finer texture, belonging to the
Frodsham beds, at no great distance from the same locality. The
Lower Keuper cupreous sandstones of Alderley Edge, Cheshire, are
frequently made up of quartz crystals on which still more minute
crystals of vanadinite may sometimes be distinguished by the aid
of a lens.
In many localities the quartz pebbles occurring in crystalline
arenaceous rocks have their surfaces, and more particularly their
upper surfaces, covered by minute crystals of that mineral. ‘This
may be observed in the case of pebbles found in Lower Keuper
sandstone in a quarry near Litherland.
At Dymoke, Worcestershire, there is a Lower Keuper sandstone
which is sufficiently coherent to admit of the preparation of thin
sections. This is a fine-grained, quartzose, distinctly DALES
rock, of which the component grains sr
in diameter. These to a large extent consist of quartz, Jeena:
enclosing hair-like crystals of rutile, and occasionally fluid-cavities,
in some of which bubbles were observed. A certain amount of
felspar, a portion of which is triclinic, is present in this rock. A
few flakes of colourless mica, and a little of the- fibrous mineral
which has been referred to as often occurring in the cement of
certain sandstones, were also observed. The cementing material,
which contains a little kaolin, encloses a few minute garnets, and
is frequently stained by hydrated ferric oxide.
The Waterstone beds belonging to this series enclose numerous
angular fragments of dark-coloured slaty rock, some of which are as
much as 3 inch in diameter. The quartz grains, many of which are
; inch in diameter, are usually much ‘younded, and not unfre-
quently enclose fluid-cavities. In addition to quartz and the
cementing material felspar is present, as is also, in small quantities,
another mineral of a light yellowish-green colour, which I have
been unable to identify, but which occasionally forms part of the
cement.
A fine-grained sandstone of Upper Keuper age, which occurs at
High House, Warwickshire, is to a large extent composed of quartz
erystals, while a bed of loose sand, found 25 fect below the surface
at Frodsham, above the Keuper Marl, is, on the contrary, entirely
made up of much-rounded grains.
The rounded quartz grains of Triassic sandstones, when examined
in a suitable medium, after the removal of their external ferruginous
coating, are found to be colourless and often transparent. Grains con-
teens ‘fluid-cavities are comparatively rare, but they are apparently
more numerous in the Keuper sandstones than in rocks of Bunter
age. <A few crystals of schorl occasionally present themselves in the
quartz of these rocks, which is not unfrequently rendered turbid
by the enclosure of what is probably a little ferruginous clay. It
is, however, probable that the grains containing “fluid-cavities in
16 J. A. PHILLIPS ON THE CONSTITUTION AND
which crystals of schorl are also found owe their origin to a different
source from. that whence the supply of quartz which does not contain
such cavities was derived.
Jurassic.—A fine-grained Upper Lias sand, of a greenish colour,
from Seizincote, Stow-on-the-Wold, Gloucestershire, effervesces
when treated with hydrochloric acid, leaving grains of transparent
quartz, which are generally angular. In some instances, however,
their more acute angles appear to be slightly rounded, although
the mean diameter of the fragments is only 5,5 inch. Besides
quartz containing occasional fluid-cavities, usually without bubbles,
there are present a few pieces of somewhat.doubtful felspar, together
with numerous fragmentary crystals of schorl and garnet.
The only coherent arenaceous rock of this age which I have had
an opportunity of examining is that quarried at Egton, near Whitby,
under the name of “‘ Moor Grit,” which is locally much employed
for road-metal. It is white and fine-grained, being often so
compact as to be entitled rather to the name of quartzite than to
that of grit. Its geological horizon is above the Grey Limestone in
the estuarine series of the Lower Oolite in North-east Yorkshire.
Under the microscope this rock is seen to be almost entirely
composed of CSIDENEDE, colourless quartz, of which the largest
pieces are about -; inch in diameter, and of which the ineleal are
usually more or. less removed. Around and between these grains
a deposit of transparent crystalline quartz has taken place, thus
forming a cementing medium. A few small garnets are present,
but no “fluid- cavities ath bubbles were observed, although some of
the quartz encloses minute crystals of a yellowish mineral which
I have been unable vo identify ; these are exceedingly minute,
often not exceeding ;>4y)5 mch in length. Many of the smaller
grains in this rock exhibit, when examined in polarized light, that
complex structure so frequently observed in the quartz of clay-slates
and other somewhat similar rocks.
A sand resulting from a disintegrated Portland Stone at Fonthill
Giffard, Wiltshire, is largely composed of ovoid grains of calcite.
After being attacked by hydrochloric acid, a rounded quartzose sand,
amounting to about one quarter of the total bulk of the mixture,
remains behind. This sand, of which the grains vary from =), to 545
inch in diameter, contains but few fluid-cavities, and these, as a rule,
are without bubbles. The fragments of quartz are associated with,
and not enclosed by, the ovoid grains of calcic carbonate.
Cretaceous.—The Tilgate Sandstone, Ashdown Sands, from Mewaee
Park, Sussex, 1s composed of slightly rounded grains of colourless
transparent quartz, united by a cement consisting partly of calcic
carbonate and partly of flint. The quartz is almost entirely free
from fluid-cavities, but encloses a few hair-like crystals of a mineral
which is probably rutile. If felspar be present it has become too
extensively altered to admit of identification. i
Sections have been examined of the chert known as Sevenoaks
Stone, as well as of several others of Lower Greensand age. They
all contain numerous fossils, particularly sponge-spicules, and in
HISTORY OF GRITS AND SANDSTONES. 17;
some cases consist, to a large extent, of amorphous silica; in others
the rock becomes crystalline and distinctly chalcedonic. The flinty
varieties often contain crystals of calcite, which cluster around an
included fossil as a nucleus. All the specimens examined contain
glauconite, and occasionally grains of ordinary quartz, some of which
are much rounded, while others are angular.
The “‘ Carstone” of Hunstanton, near King’s Lynn, Norfolk, and
of various other localities, is a friable ferruginous sandstone belonging
to the upper portion of the Lower Greensand formation, and occurring
in beds of which the relations have not, as yet, been accurately
determined. A series of specimens from this locality was kindly
furnished me by Mr. 8. B. J. Skertchly, of the Geological Survey,
who is at present occupied in working out the geology of the district.
With the exception of certain variations in colour, these beds so
closely resemble one another in their general characteristics that a
description of one of them will suffice for the present purpose.
A specimen of Carstone from immediately below the Red Chalk
exposed in the cliff at Hunstanton was found to be mainly composed
of a mixture of somewhat rounded grains of quartz, with small
pebble-like granules of dark-brown iron-ore. The individual grains
of these minerals vary in diameter from +4, inch to the most minute
sand, although small pebbles of larger size than the highest limit
quoted are not of unfrequent occurrence. The quartz contains
schorl and rutile, together with a few fluid-cavities, of which the
majority are without bubbles. In addition to ordinary quartz
grains, this rock, when carefully disintegrated, exhibits numerous
examples of the angular bodies resulting from the breaking-up of a
siliceous deposit formed between the grains of the original sand,
which have been noticed (p. 13) in connexion with millet-seed
sandstones of Bunter age.
By the prolonged action of hydrochloric acid the quartz of this
rock is rendered colourless, while the globules of ferric hydrate are
dissolved, with the exception of a siliceous skeleton which preserves
the exact form of the original grains. These bodies do not usually
exhibit colours when mounted in balsam and examined by polarized
light; but in a few cases the presence of a dark cross indicates a
pisolitic structure in the siliceous residue*. In addition to the
foregoing, this rock contains a few minute scales of mica and a very
small quantity of felspar. The majority of the grains of quartz
have their angles distinctly abraded; in some instances they
have been completely removed, and a pebble-like form has been the
result.
A specimen of Carstone obtained from a bed directly beneath the
Red Chalk, afforded on analysis the following results :—
* Both Dr. Percy and Professor Judd have described siliceous skeletons which
occur in the pisolitic grains of Northamptonshire iron-ore:—Metallurgy, Iron
and Steel, pp. 225, 226; Memoirs of the Geological Survey, Geology of Rutland
&e. p. 119.
@.5.G.S. No. 145. C
18 J. A. PHILLIPS ON THE CONSTITUTION AND
Ao [fab PeTRONINE TLIO 54 ooo 55.0 v 3°85
Water (eee CEG dire a ok 6:56
SiGe hy he SeGec Peat tice eee engin A981
Phosphoric anhydride yee eee 0-42
PAWL UUAAATN Gute we loy nee Rete es eRe ee ene eC Salen
*Reric Oxide y tea ena eee 29°17
errous OxIde « Yds sie: 0-35
APART) A eee) Seat a ee aaa i ocean a 2°43
Macon esiae Ac eeciee cea ee Reet ee 0°95
POEASSA EL. Sei ie Reale 0°48
SOdariicls eae Re Ray erp acters 0-84
100-03
Another variety of this rock from the same locality, but darker
in colour, was found to contain 37 per cent. of ferric oxide and 4o
per cent. of silica; the amount of phosphoric anhydride was nearly
the same as in the first specimen analyzed.
An examination of the spherules of various pisolitic iron-ores
shows that they exhibit all the characteristics of the globular
ferruginous grains found in these sandstones; and it may therefore
be inferred that they have had a similar origin. A pisolitic iron-
ore of Middle Neocomian age, which occurs at Market Rasen in
Lincolnshire, consists to a large extent of spherules very closely
resembling the ferruginous grains in the sandstones at Hunstanton.
Tertiary.—Hertfordshire Puddingstone, Lower Kocene, is a conglo-
merate of flint pebbles united by a concrete consisting of fragments
of transparent quartz and greyish flint held together by a flinty
cement. In this concrete the quartz is considerably in excess of
the flint, and sometimes contains fiuid-cavities. Its fragments are
all angular, and vary in diameter from =, to 54, inch.
A specimen of sand from Hordwell, Hampshire, equivalent in age
to the Headon beds, contains no recognizable felspar. All the quartz
down to a diameter of +, inch is completely rounded; and even the
smallest particles have had their angles entirely removed. Fluid-
cavities with bubbles are abundant in some of the quartz consti-
tuting this sand.
Sand from the Marine beds, near the top of the Hempstead series,
Isle of Wight, was, after treatment with hydrochloric acid, found to
be composed chiefly of grains of quartz, of which about three
fourths had a diameter of less than 4, inch. These, down to the
finest particles, are much rounded, although still roughly retaining
the form of the original fragments.
The fine-grained brilliantly coloured sands at Alum Bay, Isle of
Wight, of Upper Eocene age, usually classified as Lower Bagshot,
have not, as yet, been definitely identified with the beds of the London
Basin. By digestion in hydrochloric acid the quartz becomes colour-
less; and, although not completely rounded, the angles even of the
smallest fragments have generally been modified by attrition. Fluid-
cavities are not plentiful, and when present seldom enclose bubbles.
HISTORY OF GRITS AND SANDSTONES. 19
Needle-like crystals of schorl are sometimes enciosed in this
quartz.
The most considerable bed of sand at Bovey Heathfield, Devon-
shire, no. 27 of Mr. Pengelly* (Miocene?), consists largely of
quartzose fragments, nearly all of which are sharply angular, trans-
parent, and colourless. ‘They contain fluid-cavities with bubbles ;
but the latter appear to be less numerous than in the quartz of some
Cornish granites. Schorl is present in considerable quantity, both
as detached crystals and as portions of crystals, also as needles
penetrating quartz.
Post-Tertiary.—Sand washed from the Lower Boulder-clay at Holy-
well, Flintshire, is largely composed of small quartz pebbles, rounded
grains of various felspathic and other rocks, and numerous fragments
of millet-seed sandstone. A few unworn quartz crystals resulting
from the disintegration of crystalline sandstones, and some angular
grains of quartz, were also observed. Even the smallest particles of
this sand are often rounded.
The larger grains of a sand of Middle Glacial age which occurs in
this locality are either rounded grains of quartz or of some other
rock, or small pebbles of millet-seed sandstone. Those of medium
size are millet-seed quartz grains, mixed with a few unworn crystals
and angular pieces. of the same mineral.
A specimen of Middle Glacial sand from Bagilt in the same
county differs in no respect from the foregoing, excepting that
erystals of quartz derived from crystalline sandstones are rather
more numerous, angular fragments are less rare, and broken millet-
seed grains are of more frequent occurrence.
The Middle Glacial drift at Colwyn Bay is mainly composed of
small pebbles of various rocks, principally of quartz, with a few
unworn crystals of the same mineral, resulting from the disintegra-
tion of sandstones. In this drift the smallest fragments, although
generally rounded, have not been converted into minute pebbles.
At different times I have examined numerous specimens of recent
water-borne sands. Among these, that on the sea-shore at Pentewan
in Cornwall is, as described, p. 24, perfectly sharp and angular, as
is the sand on the beach at Par, about six miles further east. Accord-
ing to Dr. Sorby such is also the case with regard to the sands of
the modern beach at Scarborough, and those of the river-terraces at
Dunkeld.
A large proportion of the quartz in the sands of the Thames
valley is sharply angular, although mixed with rounded grains of
the same size. The grains of the auriferous sands collected on the
coast of Northern California are hkewise for the most part angular,
although perfectly rounded ones are at the same time present.
Among the blown or eolian sands which have been examined is
one from the Great African Desert, and another from Arabia
Petrea. The grains of these are, without exception, much worn;
and there is no admixture of the angular fragments found in
we
* “The Lignites and Clays of Bovey Tracey,” Phil. Trans. 1862, vol. clii.
p. 1019.
c2
20 J. A. PHILLIPS ON THE CONSTITUTION AND
all subaqueous deposits; the majority are in the state of minute
well-rounded pebbles. As in the case of water-borne sands, the
effects of attrition are more conspicuous in the larger fragments
than in the smaller ones; but even the most minute particles are in
these sands much rounded. Exceptionally the quartz encloses
fragments of a felspathic material; and fluid-cavities with bubbles
are not entirely absent in African specimens.
A bed of sandstone, said to occur in a salt-producing district
sixty miles south-east of Tebessa, of which some years ago I brought
a specimen from Tunis to London, is entirely made up of rounded
orains. In that respect this rock resembles the millet-seed sand-
stones of Lancashire and Cheshire; but it is unlike them, inasmuch
as no crystals of quartz, or of any other mineral, have been deposited
upon the surfaces of the rounded granules.
Modern blown sands, of which we have numerous examples in
this country, differ from desert sands and from those of certain
sandstones only in being usually somewhat less completely rounded.
Among the sands of this description which have been examined are
specimens from the dunes at Rhyl, Flintshire, Colwyn Bay, Den-
bighshire, Lytham, Lancashire, and from Perranzabuloe and Lelant,
in Cornwall. Speaking generally, the sands from the northern loca-
lities have been more completely rounded than those from Cornwall,
and consist of a mixture of worn quartz and various slaty and
other rocks, with a little felspar and a few fragments of shells.
Fluid-cavities with bubbles are rare in the quartz of these sands.
In addition to rounded grains of various slaty and other rocks,
quartz, felspar, and fragments of shells are present; among these
quartz largely predominates. The Cornish sands contain a few
partially rounded prisms of tourmaline.
Chemical Composition of Sandstones §c.—A microscopic examina-
tion of a large number of sections of grits and sandstones haying
led to the conclusion that many of the published analyses of such
rocks must be of a very imperfect character, five different specimens
were selected for analysis.
In making these analyses I have received the valuable assistance of
Mr. E. W. Voelcker, A.R.S.M.; and in each case fusion with alkaline
carbonates was adopted. The estimation of alkalies was made after
an attack by hydrofluoric acid, and was checked by a fusion with
carbonate of calcium and chloride of ammonium.
HISTORY OF GRITS AND SANDSTONES.
PAA
Analyses*.
I. 1 III. TV. V.
Winter { hygrometric ...... 125 150 050 “400 150
Combined) J/.05.5-.+- ‘935 “700 | 1:290 "850 "300
STLE ES) coo Ogee See 80-600 | 75°750 | 87-400 | 85:550 | 87-150
ALOT eee ee eee 9200 | 8227 | 3997 | 7570| 3-948
Carbonic anhydride ......... IE OZON ers cce IES7Oa | iecsaccc: 1-200
Phosphoric anhydride ...... ‘076 0-15 | trace. 070 | trace.
Sulphuric anhydride ...... trace. 171 060 | trace. ‘094
IEEEIGIOXICO) -o 20... 20. -c25e0e- trace te LO ile rsa leases ses 1-352
IERCOUSIORIGE ........5..002- 2370 1352 1366 1-915
Herre persulphide (ReS,) .|....2..5. | ..-..---- 800 ‘73 °203
Manganous oxide ............ 232 | trace. PALS) A paceoagee
IDEID® 48-0 /0dsseeeee ee 1-330 532 1-932 588 | 2°681
WEEN GEIC)) ieee en oe 1-285 "360 684 612 1-080
I°QUSINEC) SASe nae ROneeee pe eeeeeee 1-647 1-059 Weal "915 1:273
SG)” cocccseeCsn senate USB | es} "332 | 1-113 "840
100-197 | 100-120 | 100-307 | 100:336 | 100-271
Specific gravity ......... 2-689 | 2-464 2710 | 2-531 2-660
J. Grit, Cambrian: Barmouth, North Wales.
II. Sandstone, Carboniferoust: Yoredale Series, Shalk Beck, Cumberland.
Iii. Sandstone, Carboniferous: Millstone-Grit Series, Brigham, Cumberland.
IV. Sandstone, Carboniferous: Lower Coal-measures, Spinkwell quarry,
Bradford.
VY. Sandstone, Triassic: Bunter, Bootle Well, Liverpool.
Examination of Water- borne Sands.
With the view of to some extent studying the action of running
water upon the mineral fragments which it transports, a microsco-
pical examination was made of the sands of the St. Austell river, in
Cornwall. This stream, which during the summer months is a mere
rivulet of moderate size, sometimes in winter becomes a considerable
torrent. Its eastern arm arises at a distance of two miles and
three quarters from the town, and at a height of 470 feet above the
foot of the weir at the “Old Bridge.” Its western arm, which meets,
the other a little north-west of the town, takes its rise in a small
valley only a mile from the point of origin of the more easterly
branch. From the bridge the distance to the sea at Pentewan is
four miles, while the total fall is only 114 feet.
This stream formerly carried with it into the bay vast quantities
of the granitic sand which is separated by washing from china-clay
at the different clay-works in the district. As, however, catch-pits
have of late years been employed for the purpose of retaining it at
* Since the above were completed, my attention has been directed to some
analyses published in U.S. Geol. Survey, XLth Parallel, vol. ii. pp. 35 & 246,
which agree very closely with those here given.
+ A white fine-grained sandstone, much spotted with brown. -
22 J. A. PHILLIPS ON THE CONSTITUTION AND
the several works, the quantities thus transported are now very
small.
On the eastern branch a certain amount of granitic sand escapes
into the stream almost immediately at its source; this is repeated
at short intervals for a distance of a mile and a half, and finally
ceases a mile and a quarter above the Old Bridge, at a height of
about 200 feet above the weir-foot.
The first introduction of sand into the western branch takes place
nearly a mile below its source, and is discontinued half a mile
further down its course, but at a somewhat lower level than in the
case of the eastern fork.
It follows that, before arriving at the bridge, each grain of sand
must have travelled over a distance of at least a mile and a quarter,
with a fall of above 150 feet, while a portion of it has been trans-
ported two miles and three quarters through a channel thickly
strewn with granite boulders, and having a fall in that distance of
470 feet.
Before arriving at the sea, therefore, the whole of the sand must
have travelled at least five miles and a quarter, with a minimum
fall of about 270 feet, while a portion of it will have been transported
a distance of six miles and three quarters over a total declivity of
584 feet.
The first samples of material were collected from the bed of the
river a little below the bridge, and a mile and a half from the point
at which the last granitic sands are discharged into the stream.
For the purpose of facilitating a microscopical examination of
these sands, they were divided into four different parcels by a series
of sieves, the first sieve allowing to pass through it all fragments
less tesa =|, inch in diameter, the second those haying a less diameter
than 4 inch, and the third all particles having a smaller diameter
fo} Wi
than —~ inch.
The lar rgest fragments, retained upon the coarsest sieve were about
7 inch in inmeten eraduating to a diameter of =, inch.
This sand consists of a mixture of quartz, felspar, schorl, and
mica, in which the last-named mineral is present in smaller pro-
portion than any of the other minerals. When examined by re-
flected light, and magnified 20 diameters, the edges and points of
the different fragments of quartz and schorl are found to be sharp
and unrounded ; the only exception being in the case of certain
grains of quartz, which Dr. Sorby suggests may have been corroded
by the action of alkaline waters, but which may have perhaps never
possessed other than rounded outlines.
The angles and edges of the felspar and mica are, on the contrary,
distinctly ‘Tounded ; and although this might have been anticipated
as regards the mica, it is at first’ sight not so easily understood in
the case of felspar, whose density and hardness differ but slightly
from those of quartz. It must, however, be remembered that the
grains of felspar had become externally kaolinized while still form-
ing an integral portion of the decomposed granite, and that, on the
HISTORY OF GRITS AND SANDSTONES. 23
removal of this coating of china-clay by washing, a rounded central
nucleus will remain.
Sand which had passed through the ;5-inch apertures of the first
sieve, but which was retained by the ,-inch openings of the second,
has a similar composition to that of coarser grain. The quartz and
schorl are both angular; the felspar is more rounded than the quartz;
and the mica, which is more plentiful than in the coarser sand, is
much worn on the edges.
The sand, which after passing through the j,-inch sieve was
retained on the ,1,-inch sieve, consists of a mixture of angular
quartz, unworn crystals of tourmaline, grains of felspar (some of
which are rounded) and flakes ‘of mica (which are much worn on
the edges).
An examination of the material which passed the sieve having
apertures ;}, inch in diameter, shows that its grains are entirely
unwaterworn. The proportion of mica is much larger than in the
coarser sands, and there is less felspar; but most of the grains have
had their angles removed. ‘The quartz is generally in the form of
tabular flake-like fragments, while the schorl often oceurs as small
acicular crystals.
The quartz of these sands is frequently penetrated by needles of
schorl; and when mounted in balsam it is seen to be full of fiuid-
cavities containing bubbles—in this respect differing entirely from
the quartz of the Cornish grits, as well as from that of the majority
of sandstones.
Specimens of the sandy deposit were taken from down the course
of the river, at intervals of a mile apart, the last having been obtained
at a point slightly above the sea-level at high water at Pentewan.
In every case, however, they so exactly resembled those first taken
from below the Old Bridge at St. Austell as not to require detailed
description. The quartz and schorl are angular, the felspar is more
or less rounded, and the larger flakes of mica are worn at the edges.
With regard to the distribution of sand along the river-bed, it is
needless to remark that the coarser fragments are found towards the
centre of the stream, while the finer silt, with minute flakes of mica
and quartz, accumulates in less rapidly moving currents near the
banks.
Having found that quartz grains below —4, inch diameter are not in
the slightest degree rounded by a minimum transit of five miles
and a quarter down the course of the stream, it was thought desirable
to ascertain the effect of a prolonged action of the waves upon the
sand lying on the sea-shore.
It must be here remarked that since the first opening of china-
elay works in this district, now about sixty years since, millions of
tons of granitic sand have been carried into the sea by the streams
into which it was discharged. The effect of this at Pentewan has
been to silt up the harbour to a very serious extent ; while the whole
of the sands upon the sea-beach bear evidence of having been
derived from the same source.
The point from which the specimens were taken for examination
94. J. A. PHILLIPS ON THE CONSTITUTION AND
is situated at a distance of half a mile west from the present mouth
of the stream by which the sands were brought down. They were
collected from the water’s edge at half-tide; and as the discharge of
granitic sands into the river has been very small during the last ten
or twelve years, and this point is considerably removed from its
mouth, it is evident that a large proportion of the grains taken must
have been subjected during many years to the wearing action of the -
waves.
An pao of this sand shows that quartz having a diameter
between =} go and zy 5 inch is usually angular, although some of the
larger pieces are “distinctly (but not considerably). rounded. The
schorl, like the quartz, generally” presents sharp angles, although
somewhat abraded grains ‘of this mineral are occasionally met with.
Nearly all the felspar is rounded to a considerable extent, as is also
the small Graal of mica which is present.
Below =; inch in diameter the angularity of the fragments of
quartz and schorl is perfect, with the exception of ‘occasional
‘ corroded ” grains ; the felspar has, for the most part, rounded
outlines; and mica is almost entirely absent.
At page 32 of his Address to the Geological Society of London
(1880) Dr. Sorby remarks :—“ Unfortunately I am not acquainted
with sufficient facts to prove how long it would require to thoroughly
wear down and round a grain 4, inch in diameter. It is evident it is
avery different thing from the wearing of a pebble, and may require
a longer period of wear than we might suspect, if we did not bear
in mind that when buoyed up by water the friction of such small
particles on the bottom must be always small.” Again, at page 34,
he says :—‘‘ It appears to me sufficiently proved that a great amount
of drifting and mechanical action must be segue to wear down
angular fragments of quartz into rounded grains 7 )q inch i in diameter,
ith i have taken as the standard for comparison.”
Professor Daubrée states that the diameter ot erains capable of
floating in slightly agitated water is about 4, millimetre, or, say,
sti inch, and remarks that all smaller grains must of necessiby
remain angular *. He subsequently says ‘That a current or wave
capable of carrying off in suspension particles of that diameter, with-
out in any way affecting their form, would cause larger fragments
of the same mineral to so rub one against another as gradually to
produce rounded sand. According to an experiment quoted by this
STN, a sand of which the grains have a diameter of ;°, millimetre,
say =, inch, to which a movement of one metre pe Tagan 1s Im-
ee becomes rounded, with a loss equal to 754 pp of its weight
per kilometre traversed.
This experiment appears to indicate that a grain of quartz zy inch
in diameter requires, before becoming completely rounded and
assuming the form of a miniature pebble, an amount of abrasion
equal to ‘that which would result from having travelled a distance
of three thousand miles. In arriving at this conclusion the fact
must not be lost sight of that, after the first rounding of the
* Géologie Expérimentale, p. 256.
HISTORY OF GRITS AND SANDSTONES. 25
angles and edges, the operation will gradually become slower as the
surfaces become more worn and the weight of the grain decreases.
That angular fragments of quartz having a diameter of less than
=i; inch remain unrounded by the continuous action of breakers after
many years’ exposure, is evident from an examination of the sands
at Pentewan. It has been shown by other evidence, as well as by
the recent experiments of Professor Daubrée, that the rounding-down
of such sands by the action of running water must be an exceed-
ingly slow operation, and one requiring a somewhat active current
with an amount of friction equivalent to transport over enormous
distances. Grains of quartz of similar dimensions are, in blown
sands, completely rounded.
Summary and General Conclusions.
The Cambrian grits of Barmouth contain quartz and felspar, both
in the form of angular fragments and also as rounded pebbles. The
materials presenting these different forms have probably been de-
rived from two distinct sources; while the large size and complete
sharpness of the angles of mauy of the irregular grains appear to
indicate that they cannot have been transported from any consider-
able distance, and that the felspar cannot have been derived from
kaolinized granite.
All the arenaceous rocks of Silurian age which have been ex-
amined contain a small proportion of felspar, the grains of the
various constituent minerals being in some cases angular, and in
others rounded.
Many of the rocks belonging to this period are composed of a
mixture of grains of both forms. Among rocks mainly composed of
rounded grains are the Stiper Stones of Shropshire and the Lower
Lickey Quartzites of Westmoreland. Some of the grits from the
neighbourhood of Aberystwith enclose fragments of a volcanic rock
of doleritic character.
The grits of Cornwall, which are of at least Devonian age, include
flakes of soft slaty rocks, the edges of which are perfectly sharp,
together with angular fragments of the well-known “ greenstones ”’
and ‘‘ dunstones” of that county.
A large number of the Carboniferous, Permian, and Triassic
sandstones are composed almost entirely of quartz crystals, which
have undoubtedly been produced in sztu, as they not only penetrate
and interpenetrate one another, but also exhibit the most perfect
sharpness and freshness of outline. As confirmatory of this hypo-
thesis it may be mentioned that in a quarry at Foggen Tor, on
Dartmoor, the felspar has in places become decomposed into soft
kaolin, in which the liberated silica is imbedded in the form of
ageregations of well-formed and transparent quartz crystals *.
Unworn double-pointed crystals of quartz, likewise resulting from
the decomposition of felspar, have. recently been found near St.
Austell, Cornwall, in soft china-clay; one of these, more than three
* Quart. Journ. Geol. Soc. vol. xxxvi. p. 9.
26 J. A. PHILLIPS ON THE CONSTITUTION AND
inches in length, is now in the collection of the Museum of Practical
Geology. Sandstones of this description are not unfrequently with-
out any kind of cementing matrix, being merely felted together by
a matted intergrowth of their constituent crystals.
Professor Daubrée entertains the opinion that crystalline sand-
stones frequently owe their origin to chemical agencies resulting
from an outpouring of igneous rock; but, although this may some-
times haye been the case, many of the most completely crystalline
British sandstones are situated at distances of many miles from any
known rock belonging to this class. The same author maintains
that the presence of anhydrous ferric oxide in sandstones affords
evidence of their having been subjected to a high temperature*. It
must, however, be remembered that the carnallite of Stassfurt, which
has evidently never been highly heated, contains crystals of specular
iron-ore.
Numerous fine-grained sandstones, particularly among those of
Triassic Age, are composed of quartz grains so completely rounded
as, under the microscope, to resemble well-worn pebbles. These
‘* millet-seed”’ sandstones are often coloured either red or brown
by variously hydrated oxides of iron; and in some cases minute,
perfectly formed, and beautifully transparent crystals of quartz have
been developed upon their surfaces.
On attacking the sand of such sandstones with hydrochloric acid,
the oxide of iron is easily removed, put the crystals of quartz still
remain firmly attached to the surface of the grains upon which they
have grown. It would also appear that crystals have been formed
upon those parts only of the grains which, having been free from a
coating of oxide of iron and from every other extraneous material,
have admitted of direct chemical contact between the silica of the
rounded quartz and that of the subsequently formed crystals.
In addition to silica in the form of perfect crystals of quartz, that
substance has often been deposited in such a way as to fill cavities
existing between the original grains of sand.
As this silica has frequently been thrown down upon a thin deposit
of ferric hydrate, it is generally detached by prolonged digestion
in hydrochloric acid, by which the intervening ferruginous coating of
the grains is ultimately removed. When such a deposit of silica
adheres to only one of the adjoining grains it may give rise to a de-
pression upon its surface of the kind represented in fig. 4, Pl. II.
On examining a considerable number of modern sands, none of
them, excepting such as had long been subjected to the wearing
effects of wind action, were found to resemble those of the millet-
seed sandstones in having all their grains reduced to a pebble-like
form. Among these the grains of blown desert-sands most com-
pletely resemble those of millct-seed sandstones.
* Géologie Expérimentale, pp. 226-230.
+ With regard to the Torridon Sandstones of the Central Highlands it has
been observed by Professor Bonney that wherever “dirt” has been deposited
upon the siliceous grains their agglutination has been prevented (Quart. Journ.
Geol. Soe. vol. xxxvi. p. 106).
HISTORY OF GRITS AND SANDSTONES. 27
The above facts would appear to render it probable that the
rounded grains of these sandstones may be of eolian origin, and
that, during certain periods of Triassic time, desert areas with blown
sands extensively prevailed in this country.
Mr. De Rance has observed that the millet-seed beds are usually
free from pebbles, shale-beds, pseudomorphs after common salt, and
from all traces of life*—conditions which are characteristic of de-
posits produced by wind-currents.
The granules of brown iron-ore which are so plentiful in the
**Carstones”’ of Hunstanton are pisolitic grains, and not fragments
of that mineral rounded by attrition.
An instructive example of the occurrence at the same time of
rounded and angular grains is met with in the Interglacial sands of
Flintshire, where seme of the pebbles are fragments of a millet-
seed sandstone, while many of the smaller particles are grains
detached from the same rock. .
HXPLANATION OF PLATES L. & II.
Puate I.
Magnified 18 diameters.
Fig, 1. Group of felspar crystals in Cambrian Grit. Polarized light: p. 7.
2. Grit from Ladock, Cornwall, enclosing a fragment of a volcanic rock.
Polarized light: p. 10.
Prats IT.
Magnified 100 diameters.
Figs. 1, 2,3, & 5. Crystals of quartz deposited upon rounded grains of the same
mineral in Bunter Sandstone: p. 18.
4. Depression in a grain of quartz from the same sandstone.
6. Corroded grain of felspar from the same.
7. Rounded grain of quartz with attached crystal of iron pyrites.
Discussion.
The Presrpent expressed his sense of the value of Mr. Phillips’s
communication.
Dr. Sorpy expressed his agreement with the paper, to which he
had listened with great interest, especially as the author had ap-
proached the subject from a point of view somewhat different from
his own. He was especially glad to find that his opinions were
confirmed by the author, especially as to the crystals of quartz in
certain sandstones. The observations as to the time required to wear
down a grain of sand were especially valuable. He had found the
drift sands of the Yorkshire coast almost all angular; but then those
examined by Mr. Phillips were from another locality, which might
explain the difference in their observations. He should only regard
sand as eolian when a very large proportion of grains were rounded.
* “Further Notes of Triassic Borings near Warrington,” read before the
Manchester Geol. Soc. June 29th, 1880.
28 ON THE CONSTITUTION AND HISTORY OF GRITS AND SANDSTONES.
So far as his observation had gone, the sands of the dunes on our
coasts were not much more rounded than other sands.
Dr. Hicks said that the condition of the Barmouth Grit led him to
think that the materials had not drifted from far. He had also
observed that there was a large proportion of rounded grains in
the Stiper Stones; were we to suppose these to be blown sands?
Rounded grains were still more common in the quartzites of the
N.W. of Scotland ; we must believe therefore that there was, still
remaining at the time they were deposited, an adjoining great land-
area or the materials from one not far away.
Mr. Dr Rance said that the Keuper beds under the Marls were
now divided into the Water-stones, soft current-bedded sandstones
called Frodsham beds (which denoted entirely different physical
conditions and contained the millet-seed grains), and then the Lower
Keuper building-stone (Labyrimthodon-beds). Then came a line of
erosion. In the Bunter series were the Upper Mottled Sandstones
(with the millet-seed grains), then the Pebble Beds (which had a
different kind of current-bedding from that of the Frodsham beds),
then another line of erosion and the Lower Mottled Sandstone with
millet-seed grains again. The bedding of the sandhills of Lanca-
shire much resembled that of the Frodsham and other millet-seed
beds in their high angle and rapid change.
Mr. Ruttey said he had examined eruptive rocks rather than
sedimentary, but could not but express his gratification at the
agreement between two such observers as Dr. Sorby and Mr.
Phillips. He called attention to the presence of felspar in many of
the sandstones described, and suggested that it was possible for
such sandstones to be changed into felstone. There was often
much difficulty in distinguishing between the finer-grained igneous
and sedimentary rocks. He also called attention to the develop-
ment of microcrystalline structure in felspar crystals.
Mr. Branrorp said that some years ago he had examined the
Indian desert, and found the grains of sand well rounded. They
were mostly of quartz, with a few of felspar and occasionally of
hornblende. The strongest wind there blows from the west; the
sands had come from the coast and the river Indus; and the sand
in the bed of the river was also rounded. The blown sand ap-
peared unstratified.
Mr. Puitiips said that the grains of millet-seed sandstone were
much more rounded than was usual in sea-sand. He thought the
rounding of felspar was often due to disintegration by decomposition.
With regard to Mr. Blanford’s remarks, he could only say that he
believed the grains of all the desert-sands which had been yet
examined had been found to be much rounded.
INTERGLACIAL DEPOSITS OF W. CUMBERLAND AND N. LANCASHIRE, 29
3. LNTERGLACIAL Deposits of West CumBertAnp and Norra Lanca-
sHirE. By J. D. Kenpatt, Esq., C.H., F.G.8. (Read Novem-
ber 17, 1880.)
[Puate IIT.]
CoNTENTS.
1. Introduction.
2. Observed Facts.
3. Deductions.
1. IyrrRopuction.
Tue glacial deposits of these districts are capable of a threefold
division, as below :—
1. Boulder-clay (Upper).
2. Sand, Gravel, and Clay.
3. Boulder-ciay (Lower).
Seldom do we find the whole three members present in one
section. Sometimes the Lower Boulder-clay alone is found; at
others this is overlain by sand or gravel or clay, or by some or all
of these rocks. In other cases we find the series complete. They
occur almost continuously, in more or less completeness, from the
sea-shore to an altitude of 500 feet; and from that level they appear
in patches up to 1000 feet above the sea.
The two Boulder-clays have the ordinary character, and are very
much alike, except that the lower is tougher than the upper and
contains larger boulders. ‘The character of the included stones is
the same in both clays, as well as in the middle sands and gravel.
Some most remarkable facts are presented by the distribution of
these boulders*.
Associated with these glacial beds, and occurring at various
places, sometimes inland, sometimes along the sea-coast, between
high- and low-water marks, there are a number of deposits of vege-
table matter, which hitherto have been almost entirely neglected by
geologists.
When occurring on the sea-shore, these deposits usually pass
by the name of ‘‘submerged forests.” I am, however, inclined
to doubt the accuracy of this appellation. After a long and careful
investigation into the nature of these deposits, I have come to the
conclusion that they are not forests at all, nor the sites of forests,
as will appear further on.
* “On the Distribution of Boulders in West Cumberland, by iD) Kendall,
C.E., F.G.S.,” vol. v. Trans. Cumberland Assoc. for the Advancement of Lit.
and Science.
30 J. D. KENDALL ON THE INTERGLACIAL DEPOSITS OF
2. OBSERVED F Acts.
Lindal deposit.—The first of these deposits to which I shall refer
has already been dealt with by two other writers :—
First, im vol. xvii. p. 274 of the Quarterly Journal, in a short paper
by the late Mr. John Bolton, “On a Deposit with Insects, Leaves,
&e.” ; secondly, in vol. xix. p. 19 of the same Journal, in a paper
by the late Miss Hodgson.
A comparison of these papers will show that the writers differed
seriously about the facts with which they dealt. It is therefore not
surprising that they arrived at very different conclusions.
Owing to this discrepancy, I have been at some pains to ascertain
the facts accurately ; and I give them below.
The position of the deposit referred to by the above writers is shown
on the map (Plate III. fig. 1). It occurs near Lindal in Furness. In
figs. 2-4 a plan and two sections of the deposit are given. The data
from which these sections were prepared are given below; they
were obtained by a number of shafts and boreholes put down by
the Ulverston Mining Company in search of hematite. The posi-
tions of the boreholes are shown in the plan and sections.
Sections of Boreholes.
(Explanation of local terms used :—Pinel = Boulder-clay ; Black muck* =
Vegetable deposit.)
Borehole No. 41.
Thickness Depth
of each from
stratum. surface.
ft. 1. Tt, iA.
Surface=soilk i. 25. cab onteenic an eee eee: 2 0 2 0
Gikey spinel. seas <hq. came cteetiannste duets ease 66 0 68 O
Iimestone. ce fhe eceeeseee cee eee 29 O 97 0
Borehole No. 42.
Stttace-soil: | Sea ey eee eee ane 1) 1 O
Inte lay’ | L.. ca beset hee ae eee 3 0 4 0
Gravel:andustones a peeeee ree eee eee eeeee 20 O 24 0
Borehole No. 48.
Surface-soil\ 722 aeece ae eee eee 1) 0
GEBIVEL 256 oe nonce ee ee ee i @ 2 0
Blue clay iii ee ee ei 8G o 6
Pinel (blue) he eee eee 4 0 <1 6
GAVE aco cacac cs ty gas Cee ee 9 O 16 6
Gravellypimel 9). ees. eee ee ee eee 10 O 26 6
black aniwek (woody) ss. © (5
Blue Sarid 4.) a be 4 0 35 «6
Grey. pine .2....85. 052 eal ee ee 5) 20) 40. 6
MMMES TONE xy..::ideseteoteet cee Eee 2 0 A? 6
Grrevajoimel i.) .0. Ges. anne eee 10 O 52 6
Jointy limestone ....... waleie sa Gee 28 0 80 6
MM c . .
_* The use of the term ‘Black muck” is here clearly wrong, but quite a
pardonable mistake for a borer to make. “ Black muck,” as that term is
usually understood in Furness, does not contain any vegetable matter.
2
WEST CUMBERLAND AND NORTH LANCASHIRE. a)
Borehole No. 44.
Thickness Depth
of each from
stratum. surface.
Hits abale ft. ine
RECS Olan sae eee ena ae ee cose uae. 1 1 ()
ESN Gl aya 9 yee nce <a chtstecststiecsesseaa= 3 0 4 0
STENT EL yu Ae 42 le ia ee oe 18 0O ya NY)
PEPE TSLOMEH ete oe Ste eee oes cak dice ie DG
Hed RUN CM ra. ceseds-. sores osaeset mata nce res 6 O 29 6
STOW TTI ee ee ee a ene 9 0 38 6
ICE: MUCH: (WOOGY) "2 y.5-.-csceeesc ees TO 5) 6
LEE SON Lah seh ee ede eee ee pe Meri na oa 0 48 6
LGLLON? GLa -taed sc tccRe seeeees tesa esa neEn ie a0 HIG
Greys pinel) 25202... .5.)...2cses eee anaes 3.0 54 6
Reddish pinel with limestone ............ oy 62 6
REG! CLES conenee cee a eure mane ABE Eason eaenerrs 4 0 66 6
{LEIDER ATS, 5 Bape Se ee re Pn ee 22 O 88 6
SIGIUG GIR | RBRS noses eae saree nee aanee Bs AD) 91 6
Borehole No. 45.
Selb Gaecaill GE ee aan eee ei ae 113s ACG) i)
PASSE psa Soe Boba Se ana ee 220 De
aE NE a ots he le enc sc sleersaice ele ce Hae) 3f 0
IBIQCTE MUCK (WOOGY ) ..200.020+020-2 0-00-2506 200 57)
TE LIED SDUNGL TUES AS Aiea eal ee Be Rn Re foe Q 64 0
CURRIN costes. st Ween some cae seoase CW (ie AD
PREC lage es foe tees viewer ac secoe ncsecenis 10 O 81 0
LD ASTESUOIIVO. 25 SSSR AUEe BAP RPE ER BURR Apne nthe ar Ae 2050 101 O
Borehole No. 51.
IEICE STUY IAS Lk a a bp aZe'O iy otk
Meee piel os. . 525. 5. snacnnesciceccetssasseess 13 0 15 0
ISeeye MINE esis oc vastsccsessccserscccsesce) | 40> O 58 0
£2, DIG TLS Te EA ae eT 5 0 63°60
Meme CLAY, |... 2. -e- wee Laseedesanecesazserees 7; 0 65 0
Wellow SO8Sdn 2......i5<.csszszcccescsccctes 1 0 66. O
[h.20, (UNDO) UG. Ae eee ee nen Asean erate 20 ua
TCT OIHS sa cae Ae SBE aera ee eee 0 8 th ts
Drarke pinelee sco< ccc) for seed cbt eee seed eons (0) TAS
| TTT SST ROTI Ha 5, ae ee eee a 10226 88 2
Berehole No. 52
TL GGRCTOTL | 4 Bae eee ree tay See as YY) Zi
LES, TELS) eee a ie ee ee 30 0 32 0
S15) LNG) Se nee ee ae ee 36 0 68 0
TE0) (UDnelh A On reer eee ener 9 0 TD
2 SRE ETS E Gere ee ie Aa ee ee 10 O 87 O
Borehole No. 58
Brriietee SONNE och rat ee) eos oe te oo ck je car
“Sse TOG) deg ee pace eee ee SiO 82 0
22 UE TSG A Bane nee ae 20 86. GO
eilack Muck (WOOdY).......2.c-s.0s00es0s-+ 24. 0 ITO. ©
“ELISE ROTI | RA a Oe Sat Oe ee ee 20 112 @
25G7, TID MIP Nee hee cote aera ek eee ee 3 O 11d O
Red pinel and limestone .................. Dd 0 120; “0
ison ore and’ StOneS ....2...c..6+0ssececeso- 2 0 176
1 L POTTS) OTIS) gai oe eae le ae 0 10 122 10
J. D. KENDALL ON THE INTERGLACIAL DEPOSITS OF
Borehole No. 59.
Thickness Depth
of each from
stratum. surface.
ft. in. vita) 00
Gin hacessOll wh esceesoceoe en Sas ee eee 2 0 20)
(Civeyy jOMMVall, $4 Age ceoononoccdseosaso0q0esc0acuce 70 O 72 O
Pack Much (WOOdYy))..0-.2-+ ease eee ene 10 eG
Mplueusamd:) eee. va. acd. eats eee eee 2 0 75 O
BLACIEGICULCK (WOOGTY, ics): 2-- cee eeecee ene il ©) 86 oO
(Ble San yess vas she cciececeha ries mse eeeeeeee 4 0 90 O
Regine), ese qucicec ce ss one eee eee 4 0 94 0
Weimre stones. asactien seca ee cre nce eeee gy 103 0
Borehole No. 60.
Surface=soil’"... ote ccseeece scence ee eee eeee i) 0
Red Spinel. 3c pki alo dare eee 30 0 3l 0
Greyipimel ponent edocs ce coe earner ee 43 0 74 0
THAD GOOG (CiOOENS)) anncoodescosescsesnsa%a: 12 © 36 0
Bluewsand. “pe sves. cect scans cmesee cee enecene 2 0 838 0
Wellowashiclaw ero suse eee ee ce eeeeeeee 2 0 90 O
Broken ground (dragged by workings).. 22 0O ZO
Limestone \ian.cecenes eee eee cee eee 4 0 116 @
Borehole No. 61.
Surface-soil 7 ces cece eta 0 ib
Grey pinell .2) a frase aes ancien eee 69 O 70 O
Vellowapinelieereseenceceres Re, eee 20 ( Y
Grey spinel 284 4e seen se ee eee 6 0 fier
BIGche: MUch Ne die Oe eee eee eee Go) 3 S7aas
iBlnevclaya(Sandiy)) eens eee ee eeeeee eee 3 0 90 3
Limestone). ccc saanscce wer teden eae nee Oo 90 11
Redspinell #224 4: gests cere eee ee netec ene 3 0 93 11
Tumestonel. ears eee ee een eee i 94 11
Borehole No. 62.
Surface-soil’ 72. canoe eon nO ei)
Grey pinel. 2.0). eaeareeerten ae meeenaee 88 0 89 0
Black nick (woodsp\peeercceecsneeo ances If oO I0Oo oO
Blue*clay -s.i)...ccda cree eee Caen 2A) 102 O
‘Yellow sand’ \c)2) ahi ae eee eee 6 0 108 O
IRedspinelli(withtoxe) my-eetee rer eee ene 4 0 112 O
Noft stone Gwithiore)wee-eeeeeeeeeee eae 3 0 115 0
Limestone with clay joints ..............- AL MD) 156 0
Borehole No. 63.
Surtace sot: os cucacc.carel ce heeeene eee 1 A) he @
Greyopimel co. 2. ...025. ah voce eRe eee eee ay O 88 0
Black wniwek) (woody). ..2./s¢.cesanaa ete 10 Oo 98 oO
BF uSielay i athe cncea dees Ahan nea ee 3 0 101 9
ved apimell(wathyore) eee eee eee 4 0 105 O
ivedipine li (wathistone) pase -oeeree eee 8 0 113 0
iin CSLOME ransenecesscan eet ae eee eee On) ipa
WEST CUMBERLAND AND NORTH LANCASHIRE. 33
Borehole No. 64.
Thickness Depth
of each from
stratum. surface.
re aya foe ue
Surface-soil ..... ME Can Gah seen reaes eae 1 O 10)
BERG DUONG Bee dae siccncecsarciconiek asia stnies nessa 92°, 0 93 O
RICH MUCH (WOOTY) .. icccccsecesclecedenes 20 0 13 0
Bineclay ....,<.- SOLOS ROREE CNeH OAC Beare Re 2 0 Milsy
PROMEEC Ne iced wainacine Sia te oresielee eter 9 0 124 0
LEDS OT AS) GRR rey a ep Re ees f O ll 124 Li
MNOHEERIGHOMERE cas cc ccs si canaccaan ce wacscuncuces 0 8 WEY 7 /
[TRONMEGINE: SaRs AP SOG RE a ee ean LS 126 10
PROC ISLON Omen ss one ccc. tec saan tieaein 0 8 Ie 6
PEICORE ee ech escscaesewcac sec ccseeccnusl 2 6 130 O
Be ecg MM ESTOBG secs is nc wowace aaesecee' 20 0 HOO TO
SMRRESCE SOMME eonece socicceaeanieswesa oaccnaeet LG 1 O
RPE CHPNIN CY es sate ecieh Se tentisas sesaqas sins 99 0 100 O
NEGIIUGH (WOOGY))...0.2.06..00000cess00e5 AO @ 1W6) ©)
PEPER G) AY gaifoe nics chicane ce cislecicacieiviisiswesieidsis.si my AY) 122 0
SLELLORP EEOC YE ee RO 125 O
HRPM WOM Ome tes secoetecattc clas felosccetionwatloalsae 3 O 128 0
Borehole No. 66
SUREKCC-SOL Uecasccecacemerss Seacoast tak ag) 1 O
BCR CMM EG Wa aise is Sine ueueid se seeleatiina be tewans 96 0 ot 0
2r BULONTEP SENTING | So et Ts A) 98 O
EDOELIS CIES MEE RE ee 1) 116 Oo
PENITIEN SM Clere een eH Ch ecais eaten laccns wea es 2 0 118 0O
BWrellFous POSsaM” Mo. c sects tenes eat venules 6 O 124 0
TL BTIDOSTGTING Sec eie ae IS Eee ae L6G 125 6
The pinel or Boulder-clay overlying the Black muck or vegetable
matter in the above sections is the Upper Boulder-clay, having a
greyish and ochrey matrix, and containing numerous boulders, some
as much as 2’ 0" x1' 3” x1 3”; but the majority are below 3” in
diameter. Coniston grits and flags, from the adjacent highlands,
are the principal rocks represented. Besides these, however, there
are St.-Bees Sandstone, Eskdale granite, Carboniferous Limestone, &c.
The extent of the deposit has not yet been proved in cither a N.E.
or §.W. direction, as shown on the section AB (fig. 3). So far as is
at present known, it covers an area of about 34 acres.
For a list of the plants &c. found in this deposit, the two papers
above referred to should be consulted, as I had only an opportunity
of seeing some of the vegetable deposit as 1t came out of the bore-
holes. It was then too much broken up to enable me to identify
any of the plants.
Crossgates Deposits —Several deposits similar to that at Lindal
have been met with at Crossgates, in working the hematite-mines.
In some cases they were covered up by 9 or 10 fathoms of Boulder-
clay; and they invariably rested on clay. JI have seen a large
quantity of the woody matter which came from some of these de-
GedaG.s. No. 145. D
b+ J. D. KENDALL ON THE INTERGLACIAL DEPOSITS OF
posits ; but no correct information has been preserved as to their ex-
tent and thickness. Accumulations of similar material have been
met with in the solid rock, as shown in the following section :—
Section obtained by Boring at Crossgates.
Thickness Depth
of each from
stratum. surface.
fies a0 fie. nas
Soil
Danis Seer tec ate sie oars Uostasietdocioeeee aerate Het) 20
Grayeland layer. cece. s-coen cee eee 24 0 26 0
Decomposed limestone ............1--++-+-+ ge O) 43 0
Yellow clay mixed with iron-ore......... 4 0 47 O
TEUIE TUG a Me RE BORCSOE PEDO DOE ORCL EO C8.00% A (0) 5r To
Tron-ore (dark-coloured) ...........,..0++ 2,10 53 0
Black muck mixed with iron-ore......... Q, © 59 Oo
PPOM=OVC, oe cerca sh oteael cle anen acenee eee 8 0 67 20
Decomposed limestone m-.cse eeese eee os) 74 0
LEUCOE THODUY WAVOSE see cnondccodscadnacecen: 2 86 0
Decomposed limestone ........5....-....06 (ie 92 0
Black mould and wood .......2...+.0.00+00¢ oy) 94 0
Yellow clay mixed with iron-ore......... 16 0 110 O
Black mould mixed with tron-ore......... LOE 120 <0
ABU GCI I NOWLE SEN aot ee me ae ne Ly © nye)
Black mould mixed with vron-ore and
limestone
Core cesses esesaseersessesseossossseons
250 127 116
Watney Deposit—On the western shore of the island of Walney,
and about a mile south of the village of Biggar (fig. 1), there is a
vegetable deposit, in many respects like that at Lindal; but not
much of it is exposed. A plan and two sections of it are given in
figs. 5-7.
The deposit rests on Boulder-clay certainly ; but I have not been
able to prove that it is overlain by the same formation. Still I
think there is very little doubt about it when we look at the sec-
tions, and w.cen we know that the shore is travelling rapidly land-
wards. On the occasion of my visit I had not time to make any
observations on the inner nature of the deposit with the view of
determining the different kinds of plants enclosed in it; but I may
state that, externally, it is very much like other deposits that I shall
describe more in detail further on.
Drigq Deposit.—On the shore opposite Drigg (Plate III. fig. 1).
there is another woody deposit. A plan and several sections of it
are given i figs. 8-11. In one part of it I sunk a shaft, as shown
on the plan. A section of this shaft is given below.
A. Vegetable matter (brown) and grey sand in alternating layers of various
thicknesses, the vegetable matter predominating. I found in it the elytra
of beetles, acorns, oak-leaves, hazel-wood, alder-wood and leaves, stems
of common bracken, pieces of Sphagnum, seeds of various kinds and sizes,
and rush-like stems and leaves, the stems standing on end and crumpled
endwise, asif by downward pressure, the leaves lying on their side. The fol-
lowing diatoms were found in this bed:—Cyclotella minutula, Pinnularia
viridis, Pinnularia oblonga, Gomphonema acuminatum, Himantidium bidens,
Himantidium pectinale.
B. Yellow and brown sandy clay in irregular layers,
C. Blue sandy clay.
D. Red and blue sandy clay, the last 12 inches redder and more clayey.
WEST CUMBERLAND AND NORTH LANCASHIRE. 30
Some of the pieces of wood in A. were as much as 12 inches in
diameter, but all lying on their side and partly flattened as if by
pressure.
Here, as at Walney, we find Boulder-clay under the deposit, but
we have no direct proof of its having been overlain by that forma-
tion.
St.-Bees Deposit.—A few miles further north than Driggs, along
the coast, opposite St. Bees (Plate III. fig. 1), there is another
deposit, which I have examined more minutely than any of the
others. A plan and two sections of it are given in figs. 12-14.
In this deposit I have sunk several shafts and boreholes, sections
of two of which (Nos. 1 & 8) I give below.
Shaft No. 1.
A. Vegetable matter (brown) and grey sand in layers of different thicknesses.
The vegetable matter contaims seeds of various sizes, leaves and stems
of rush-like plants, hazel-nuts, leaves and wood of the oak, alder, and
hazel. The rush-like stems are numerous, and vary in length from 1
to 3 mehes; they are standing erect, and crumpled endwise, like those
found at Drigg. The following diatoms have been found in this layer :—
Epithemia turgida, Epithemia granulata, Epithemia proboscidia, Pinnu-
laria acuta. A vertebral column about the size of that of a rat was also
found in this bed.
B. Grey sandy clay containing a few rush-like leaves and the elytra of
eetles.
C. Hazel-wood, nuts, and leaves, also leaves of the oak, beech, and alder.
D. Similar to A, but containing more leaves and hazel-nuts.
(Boulder-clay.)
Shaft No. &.
A. Vegetable matter (brown), containing wood and leaves of the same kinds
as those found in the same bed in Shaft No. 1.
B. Fine oe clay with rush-like stems standing upright, and the elytra of
beetles.
C. Vegetable matter consisting almost entirely of leaves of the oak, alder, and
willow, and hazel and alder wood.
D. Brown sand and vegetable matter with some rush-like stems standing up-
right and crumpled.
On the surface of the deposit there are a considerable number of
stems of oak and alder, the former turned black and the latter
ee ; some of them are as much as 12 and 18 inches in diameter.
T also found a large piece of the stem of a coniferous plant about
18 inches in diameter. Under the microscope it was like the yew.
These stems and branches all lie on their sides. In several parts of
the deposit there are root-stocks of oak and alder with about 12
inches of stem standing, as though they had grown where we see
them: the rootlets, however, are imbedded only in vegetable matter ;
they do not extend into the underlying earth.
Near the upper edge of the shingle, on the beach, two boreholes
were put down for the purpose of proving whether or not the vege-
table deposit extended so far inland. One of these boreholes is
shown in the section A B, fig. 13. The pees of it were as
follows :—
D2
36 J. D. KENDALL ON THE INTERGLACIAL DEPOSITS OF
Borehole No. 2.
Thickness Depth
of each from
stratum. surface.
fos yaa fits yum.
Ths SIMMS Sorccsessogossscosdoopon0d0000000 1 6 LG
2, (Senne eyarsl mph yell ccooansoancanséosnc0000 Ik 3.0
By WGI QiOUG TUCIRIEP gboodbsedooonceHs50ce 3 6 11 6
4, Boulder-clay (grey) ............se0ees ROO NEG 12 0
The vegetable matter (No. 3) in this section was very soft and
spongy, easily pierced by the boring-tool, and quite unlike that found
in any of the pits or bores made on the shore, which was particularly
difficult to bore through; in fact No. 3 is more like the soft peaty
deposit which occupies the flat ground in St.-Bees valley. Two
years ago a great length of drains was cut in this peaty matter ;
and I had then a good opportunity of ascertaining the nature of it.
It, however, was nothing like the vegetable matter which occurs on
the shore, being much more spongy, and containing a far larger
quantity of water, and altogether having more the appearance of peat,
which in fact itis. The vegetable matter on the beach contains very
little, or almost no water, notwithstanding that it is covered twice
every day by the tide. Another difference between the two deposits
is that the one on the shore is quite laminated, whilst that in the
valley is totally devoid of lamination. About eighteen months ago
Pow Beck, during a freshet, diverted its course just where it passes
on to the shingle of the beach (see Section A B, fig. 13). In the
new course a large patch of peaty matter, similar to that in the
valley, was exposed. After seeing that, 1 had no doubt whatever
that the vegetable matter found in borehole No. 2 was the same, and
not at all like that found on the shore.
Maryport Deposit.About halfway between Allonby and Mary-
port, and about one third of the range of the tide from low-water
mark (Pl. III. fig. 1), there is another vegetable deposit; but it
is not very well exposed.
I have not dug through this deposit, and therefore cannot say
what is below it; and the soft silt, which covers the shore in
the neighbourhood, prevents any information on that head being
obtained. It has the same external appearance as all the other
deposits, besides being laminated and very much more compact than
peat. It contains a large number of seeds about the size of gun-
shot, and a quantity of rush-like leaves, as well as pieces of hazel
and alder wood. The wood is in every case flattened as if by
pressure. |
There is another and similar deposit about a quarter of a mile
further on the shore towards Allonby; but only the upper surface of
it can beseen. Near Beckfoot, I am told, there is another; but that
I have not yet visited ; nor have I seen one which occurs at Cardunock,
on the Solway.
All the deposits described, whether on the sea-shore or inland,
WIEST CUMBERLAND AND NORTH LANCASHIRE. oy
have the same compact nature, and, so far as I have been able to
ascertain, contain the same kind of plants.
3. DEDUCTIONS.
So little was known of the extent of the Lindal deposit at the time
Mr. Bolton and Miss Hodgson wrote, that its real geological import-
ance was missed. We now see that it is overlain by an immense
mass of Boulder-clay, in some places nearly 100 feet thick; it is
also underlain by Boulder-clay; so that I think we may fairly say it
is interglacial. The impossibility of its being a recent introduction,
carried down by means of swallow-holes, as suggested by Miss
Hodgson, must be apparent to every one now that we know more
of its extent and real nature.
We may ascribe a like (that is, interglacial) age to the deposits
at Crossgates. The deposits in solid rock were, I believe, thrown
down in preexisting cavities in the Limestone at the same time as
the deposits immediately below the Boulder-clay.
The shore-deposits, so-called submerged forests, I think are also
of the same age. We are not able to prove it so directly as in the
case of the other deposits ; but I think that a careful consideration of
all the facts must lead any one to the conclusion that they are
interglacial. The fact upon which I most rely is their compact
nature, which, to me, speaks most forcibly of their having been
subjected to great pressure, such as would be the case if they had
been overlain by the upper glacial beds. They are altogether unlike
the spongy peat which occurs in St.-Bees valley, and quite as unlike
any of the vegetable deposits which usually go by the name of peat,
although many of the species of plants found in the shore-deposits are
common to peaty accumulations.
These shore-deposits all rest on the Lower Boulder-clay, a fact
which is somewhat remarkable if they are of postglacial age. Why
should we not find some of them on the Upper Boulder-clay ?
Besides, how can it be for a moment doubted that the Walney
deposit extends below the Boulder-clay, although this has not been
directly proved. Referring to Plate III. figs. 6 & 7, we see that the
deposit dips towards the land, and that it is only about 50 feet from
high-water mark, where we have the Upper Boulder-clay. When to
these facts we add that the shore is travelling rapidly inland, it seems
to me we are bound to admit the Interglacial age of the deposit.
Usually these deposits on the sea-shore pass by the name of
“‘ submerged forests ;” but the conclusion to which I am led is, as
already stated, that they are not forests at all, nor the sites of
forests, but that the vegetable matter has been accumulated under
water. All the facts but one point in this direction: the Diatoms,
the rush-like stems and leaves (probably of a species of Sparganium),
and the interbedded layers of sand, all speak of watery conditions ;
the only fact which seems to me to indicate in any way that these
deposits are the remains of ancient forests that grew on the spot, is
the occurrence in them of a few root-stocks in their normal position.
38 J. D. KENDALL ON THE INTERGLACIAL DEPOSITS OF
But, as I have already pointed out, the rootlets from these stocks do
not pass down into the underlying Boulder-clay, but are simply
imbedded in the neighbouring woody matter. Some of these root-
stocks belong to trees which must have been at least 18 imches in
diameter; so that if such trees could have derived their necessary
nourishment from a woody soil of this kind, it is perfectly certain
they would not have been able to stand in it, because there would
be nothing of any weight or tenacity for the roots to lay hold of.
The presence of such root-stocks, it seems to me, may be better
explained by supposing them to have been floated to the positions
in which we see them. The position in which they now stand is
that of flotation; that is to say, a root-stock would be floated and
dropped in water with the same side up as when it was growing.
The inner nature of the shore-deposits being precisely the same
as that of the cavernous deposits found at Crossgates is also sug-
gestive of drifting ; for clearly the latter are not on the site of an
ancient ferest, but have been carried to their present resting-place
by water.
The facts presented by these deposits seem to me to have a most
important bearing on the question of the formation of coal. We
have here similar underclays to those which accompany cval-seams,
and the same kind of intercalated clay-bands, both of which, in the
case of coal, suggest watery conditions just as much as they do in
the deposits under consideration. I think it is just as impossible
that trees can have grown in the underclays of coal, which at the
time would be soft and inccherent, as that they can have stood in
the woody matter of the so-called ‘‘ submerged forests.” ‘The Stig- ~
maria rootlets of the coal may be accounted for in the same manner
as the root-stocks which are found in vegetable deposits like that at
St. Bees. The trees which have been found rising out of coal-seams
and passing into the overlying strata, may be explained by supposing
them to have been so loaded at the root when they were deposited
that their position of flotation was erect. In this way the whole
Coal-measures may have been deposited during a gradual subsidence
without any of the periods of cessation demanded by those who hold
that coal-seams are the remains of forests which grew in situ.
On the assumption that the shore-deposits are “‘submerged forests ”
of recent age, it has been often held that they indicate a subsidence
of the coast; and writers, in consequence, have had to make the land
rise and fall in a very remarkable and erratic manner, when dealing
with the phenomena of “raised, beaches” on the one hand and
‘‘ submerged forests” on the other. The view just enunciated sim-
plifies matters very considerably, as, according to that, the vegetable
deposits on the shore do not necessarily indicate either a rise or a
fall of the land in recent times.
}
j
|
/
|
j
}
|
|
}
|
|
|
|
>= a
SwncremavEN
etek
= 4 =
=
ae =
= \ as =>
= =
S %
so
= seice
= .
ms
iromeere Bash £ Low Water
Fig . 3.
Section on Line AB Fig 2.
Fig. 2 ae Fug. 4,
, Sectton on Line © D
Map of Lindal District ¢
wo" |
2 c Fs
ny *R , ==
[ew Te ;
\ > = AX | — 9
~ @LINDAL STATION | = -
| th
— |
: to Se £
i Se ae me ,
= 2 ( =
eee (EEN x Scale of Se 320 fe R cy
Pinna are Mineslae pur ot cale of Selon Oe 7 uh. i
: ° SUL SHAT. ‘ 4% FBedent of deposit. yt proved colored. nenlnal tint. }
MEI SHAFT \ “ 7 [||
a Ss A Grey Pinel ( Boulder Gay) Zz
x B Vegetable Deposit
C Blue Sand (Cavey)
D Red Pinel (Boulder Clav)
E
F
.
> Scale of Map 3 inches tw a Mile
_ Journ. Geol. Soe. Vol. XATVIL Pi iit
jae Ome
Plan of Deposit om Shore oppose Prigg
: Reference to Plan & Sections.
™ Figs 8-11.
A Vegetable Depostt
, B Blue Any (Sandy, )
“4 C Red Cay in some places containing stunes(Boulde Tay)
c De 3.2 5¢ |
: \ Dip of Varrane of Woody atter-
Carboniferous Limestone
Gravel
Borvholes
evel liere
Fig 1.
Section on Line €E Fig-4.
1 em A
Fig. 10
Section on Line © D. Fig.4
Agt
A
Scale of Plan und Sections AB and CD 72 feet to an Inch. :
Fig. 9. Secon on Line AB Fig. 4.
Zz
cS
f os
=
=
>
=z
oc
>
Zs:
=
Zz
aa 7
rats LINDAL
esssorr
Fig. 6. Section on Line AB Fug. 5. |
High Water __ s Eyer
eon
C Boulder Clay
A Fig. Ih.
Scale of Plan & Section AB 100 feet to an Inch SM Plan of Deposit
a y 2 ~ at S! Bees.
velerence 4
A Vegetable Deposu 1 ————
7 Glow 6 | fron ee Es SS SS \
Benet iiey . / Whitehaven; FURNESS RATEWAY
Sa
5 =
Po, !
‘sts ‘
oy = eon is /
red by Sand and 5°" er 0.47
é i , : :
SHINCLE
Fig. 5. a H rid
Plan of the Walney Depostt : {
Fig 7
Section on Line © D Fig. 5
Chaves 8
Seale of Section CD90 feet to an Inch
=
Norixontal Scale of
Reference to Plan & Sections Fig. $5 1214.
A Vegetable Deposit compact aa D® soft and spongy ke peat
B Blue Sundv Clay
C Roulder ve Sonatas Fig. 14.
D Sand & Stones covering veg le osth =
No Dep of lamina of Woody Matter eee rae Paes CEN Eee
# iP
Fig. 13. Section on Line AB Fig. R. =
ee |) ;
ot Scale of Section © DH) fet to an mck.
Hugh Water
Ww
cl Y
=== SS
Plan & Section AB Iti hes 10 a Mile
Vertical Scale cf Section AB IO feet to un uich.
MAPS , PLANS AND SECTIONS OF INTERCLACIAL
DEPOSITS OF WEST CUMBERLAND AND NORTH LANCASHIRE. -
+
Frad® Dengerlieké Leth Luratim,
=r
#
a
Final
WEST CUMBERLAND AND NORTH LANCASHIRE, 39
EXPLANATION OF PLATE III.
Plans and Sections illustrating the Interglacial Deposits of West Cumberland
and North Lancashire.
Rig. 1. Map of the district, showing the positions in which deposits of woody
matter have been found,
Figs. 2-4. Map and sections in the Lindal District.
5-7. Plan and sections of the Walney Deposit.
8-11. Plan and sections of Deposit on shore opposite Brigg.
12-14. Plan and sections of Deposit at St. Bees.
Discusston.
Mr. ©. Rem said that in the Cromer Forest bed he had dug up
many stumps of trees asserted to have been im situ, and had
found them not to be so. He thought that great caution was
needed in asserting trees to be wm situ. They would usually sink in
a vertical position with their roots downwards. Sometimes portions
of the soil in which the trees had grown were retained among the
roots, and differed entirely from the matrix.
Rey. H. H. Wrywoop pointed out. that trees often grew in a soil,
but the roots did not pierce the underlying clay. Might not this
be the case with the Cromer trees mentioned by Mr. Reid ?
Rey. J. F. Braxz spoke of a boring at York with peaty matter in
the midst of the Boulder-clays.
Mr. Tippeman asked whether it was quite certain that there was
Boulder-clay above and below these peaty deposits.
The Sxcrerary replied that the author stated so distinctly in the
aper.
: The PRESIDENT spoke of the importance of comparing together
the results of investigations in different areas. i
40 PROF. T. G. BONNEY ON THE SERPENTINE
4. On the Serpentine and assocrateD Rocks of ANGLESEY ; with a
Nore on the so-called Srrprntine of PoRtHDINLLEYN (CAERNAR-
VONSHIRE). By Prof. T. G. Bonnzy, M.A., F.R.S., Sec. G.s.
(Read November 3, 1880.)
1. ANGLESEY witH HonyHEAD IsLAND.
TE serpentine from the vicinity of Rhoscolyn, though known within
a limited area as an ornamental stone, does not appear to have
received much attention from geologists. It is dismissed in Pro-
fessor Ramsay’s memoir on North Wales in a few brief sentences,
and has not, so far as I know, met with fuller notice in any other
quarter. On the Geological-Survey map it is delineated as forming
an elongated lozenge-shaped patch about a mile and three quarters
in length from EK. to W., extending inland north of Rhoscolyn from
the west shore of Holyhead Island, and occurring in several smaller
patches on or near the opposite coast of Anglesey. In each of these
localities I have studied the rock in the field, and have examined
microscopically the specimens there collected. The results, I hope,
may be of some use, though, after three separate visits, I have not
been able to visit every one of the outcrops or examine minutely
every part of the district. Owing to the intricacy of the coast in
certain places, a map on a considerably larger scale than 1 inch to
the mile would be required before an elaborate study could be
undertaken.
The questions which I have attempted to solve (as in all former
studies of serpentine), were (1) its relations to the other associated
rocks, and (2) its nature and origin.
The ordinary rock in the vicinity of these masses of serpentine is
a dull bluish or greenish schist, composed chiefly of minutely
crystallized micaceous or chloritic minerals with some quartz, the
foliation being parallel to the bedding. The latter is generally very
distinct and sometimes exhibits very remarkable crumplings. The
serpentine occurs in low rugged knolls, cropping out here and. there
from the fields over which in the map the colour denoting its presence
is extended—the general aspect of the rock masses reminding us of
the serpentines of Cornwall, Scotland, and Italy. It differs markedly
in all its characters from the ordinary schists of the district, and,
where associated with the latter, occurs in such a manner as to
suggest either intrusion or sporadic metamorphism of a very singular
character. This is also suggested by the mapping; but it is even —
more conspicuous in the field.
My examination, however, showed me that under one name two
distinet rocks had in some cases been confounded, viz. a true serpen-
tine and a gabbro, especially in the Anglesey group. Jor instance,
if we alight at the Valley Station on the Bangor-Holyhead railway,
and follow the road to Four-mile bridge, we observe in the fields on
our left, near Ty Newydd, a long craggy mass of serpentinous
AND ASSOCIATED ROCKS OF ANGLESEY. 41
aspect, the northern edge of the largest patch in Anglesey,
according to the map. But on reaching this we find it a mass of
gabbro, generally rather coarse—considerably altered, no doubt, but
Fig. 1.—Junction of Schist and Serpentine.
! ;
\y { Ly, = t=
~ La AP ZF- : ——— Ss
AEF, SSS
GLY
Le il
——s
So :
_——DS Sq
TELL
ee Se ,
—— SS Se
a Se eee a
A. Schist. B. Serpentine. C. Sand.
unmistakable. There is, however, a small inconspicuous outcrop of
true serpentine, separated from it by some grass, about seventy yards
to the north of its eastern end. From the west end of this gabbro
massif we made* for the shore. Here we found an irregular rocky
coast-line fringed with skerries and islets, mostly dry at low tide.
Some are schist, marvellously contorted, others gabbro, a few ser-
pentine. Without a large-scale map, it would be impossible to
make the details intelligible; but it may suffice to say that we
worked carefully along the shore to the inlet by Tyddyn Gob,
examining the different rocks. In one place the evidence, though not
perhaps absolutely conclusive, seemed strongly in favour of the serpen-
tine being intrusive in the schist; for if the junction were due to a
fault, this would be a very strange one (fig. 1)7. Further on (beneath
a wall) gabbro is seen intrusive in serpentine, which has assumed,
as is not uncommon in such cases, a locally schistose aspect. <A
large mass of gabbro forms an island near here. On the bank
of an inlet near Tyddyn Gob is a rather schistose rock, which in
the lower part resembles a foliated gabbro, in the upper a schist.
Further to the south the schists are wonderfully contorted, and
there is a small mass of serpentine near Ty Ucha (reached by
crossing a causeway over an inlet); this is greatly crushed and
slickensided. Appearances suggest an intrusive junction; but both
* On my first visit to this place I was accompanied by Mr. F. T. 8S. Houghton,
to whom | am much indebted for kind help on this and a subsequent occasion.
t In the face of a crag facing S.E. and rising from the shore about the top of
the letter ¢ in mile on the map.
42 PROF. T. G. BONNEY ON THE SERPENTINE
schist and serpentine are so much affected by subsequent changes
that it is difficult to be sure.
On the north-eastern edge of this massif of serpentine (Survey
map), near Cruglas Farm, five shallow pits have been opened in a
low ridge east of the road, two being close together by the road
and outside the enclosure. In one the rock is a normal serpentine,
as it is on the right-hand side of the other; but on the left we find a
tougher variety (see below, p. 46). I failed, however, to find any
line of demarcation between the two varieties. The next two pits
are in normal serpentine, veined in places with calcite. The last is
a kind of ophicalcite, hard and tough. On my first visit I found a
loose block, near one of the western pits, of a dark green serpentine
full of lustrous erystals, up to 0-3 inch diameter, of a mineral of
nearly the same colour. I could not then discover any of this rock
ar situ, and on a second visit, after a most careful search, aided by
some of my students, was equally unsuccessful, though in one or
two places the presence of a few minute crystals in the normal
serpentine indicated a slight approach to it*. On the western side
of the road a pit has been opened in a large mass of gabbro, some
of which has a rather serpentinous aspect.
About a quarter of a mile further down the road we passed over a
reddish serpentine, rather brecciated and veined with calcite. We
again touched a little serpentine (dull green) near Gwrthya. All
the south-western end, adjacent to the shore, of the large mass near
Melin Carnau, coloured as serpentine on the map, is gabbro.
Thence we worked along the shore northward till opposite Ynyslas.
There is no serpentine here, the gabbro being succeeded by schists,
some of which are, indeed, massive and serpentinous in aspect; but
the difference is evident, even in the field, on careful examination. I
failed to find any serpentine at the shore end of the slope opposite
Ynyslas; the rock there is the green serpentinous-looking schist ; nor
did I see any in the isolated crags inland in the immediate neigh-
bourhood. The railway crosses the mass which is represented on
the map as running southward from Llyn Treflas; I walked along
this, and found nothing in the cuttings but the green schist sueceeded
by the ordinary schists of the district.
A much larger mass of serpentine than any of the above is indi-
cated on the map near Rhoscolyn, at the south end of Holyhead
island. Specimens from this locality are familiar to me; but I have
only examined the western portion of it in the field. As on the
other side of the water, both schist and serpentine crop out here and
there in rough knolls and ridges among the fields. The two most
interesting exposures are on the western side of the western of two
roads leading to Rhoscolyn. The first, near Ceryg Moelion, is a
quarry approached by a driftway. Along this we pass a large mass
of gabbro, which is succeeded by an outcrop of dark green serpentine ;
and beyond this we come to the quarry. It has been opened in a mass
* See below, p. 45, for a microscopic description.
AND ASSOCIATED ROCKS OF ANGLESEY. 43
of ophicalcite which is bordered by true serpentine on either side.
The annexed diagram (fig. 2) roughly represents the relations of the
Vig. 2.—Quarry at Ceryg Moelion.
at
Semmerene’
A. Serpentine, crushed and slickensided.
B. Ophicalcite. C. Débris.
two rocks. The boundary between them is generally quitesharp; and
the serpentine is shattered, greatly slickensided, and in parts almost
flaky, as if it had undergone great pressure. The ophicalcite varies
much: in parts nearer the edge it is evidently a breccia of angular frag-
ments of dark serpentine united by crystallized calcite ; in other parts
the latter predominates and is mottled by a green serpentinous
mineral without distinct evidence of fragments. The section is per-
plexing; but, after careful examination aided by the microscope, I
think that we have here a fissure which has been connected with
some faulting and has subsequently been filled up. As the serpen-
tine itself contains little or no lime, and as the schists of the island
are not markedly calcareous, one is disposed to attribute the calcite
to infiltration from overlying masses of Carboniferous Limestone
which have been subsequently removed by denudation.
Following the road for perhaps a quarter of a mile further south,
we pass some more serpentine and several craggy outcrops of schist,
and then in a field on the left find another interesting pit * which
has been opened in order to work a band of steatitic rock. The
annexed diagram (fig. 3) expresses the relations of these rocks.
A is a green schist with a rather high N.N.W. dip. B is the
band quarried. It is about 4 feet thick, but is rather irregular,
seemingly conformable with A, and distinctly schistose in structure.
* T believe it is called Plas Goch ; but it is most difficult to obtain informa-
tion as to names in these wild parts of Wales; the spot must be very near the
division between the two quarter sheets of the Ordnance map,
44 PROL. T. G. BONNEY ON THE SERPENTINE
Fig. 3.—Quarry at Plas Goch.
A. Green schist, well marked dip.
B. “ Steatite” schist, partially quarried out.
C. Green schist, most massive and serpentinous-looking at x.
It is very soft, like tale, and greasy to the touch, of a pale dull green
or leaden colour. C is a less pure steatitic schist, which at D
assumes a more normal character, and it dips to N.N.W. or N. xX is
more like a serpentine, and has more the aspect of an intrusive rock ;
it is of a dull-green colour, and has a slightly schisty structure, is
harder than B, but can just be scratched with the nail. It contains
numerous crystals of magnetite, commonly minute, but in places very
distinct octahedra, which are sometimes nearly 3 inch in diameter.
The matrix, however, on close examination, rather resembles a
massive chloritic rock, like some of the lapis ollaris of the Italian
Alps (e.g. that from near Chiesa in the Val Malenco) than a true
serpentine. To the latter, under the microscope, it has little
resemblance. It consists of a thickly felted mass of a scaly or
fibrous clear mineral, slightly tinged with green, and feebly dichroic.
The brightest tint shown with crossed Nicols is a dull greyish white ;
and the mineral is either hexagonal or orthorhombic; minute gra-
nules; some fairly clear, some brown to opaque, are scattered about
the slide (the larger crystals have been apparently torn out in pre-
paring it), part of which are probably chromite. After two visits
to the pit, and the best study that I can give to the rock, I am dis-
posed to think that it is more probably a massive chloritic schist
than a true serpentine, and that the appearance of intrusion is
illusory. The quarried rock (B) under the microscope exhibits a
thickly felted mass of almost colourless folia, which, in transverse
section, do not show conspicuous foliation, together with some few
scattered granules of opacite. With crossing Nicols they afford fairly
bright pink and green colours, and are almost certainly tale, so that
the rock may be regarded as a tale-schist.*
The following are the results of the microscopic examination of
some of the above-mentioned rocks. The porphyritic rock found near
* Tam since indebted to F. T. 8. Houghton, Esq., F.G.S., for the following
AND ASSOCIATED ROCKS OF ANGLESEY. 45
the quarry south of Cruglas consists of three minerals :—(a) a clear
transparent mineral, with a satiny texture and occasional very faint
indications of two cleavage-planes ; with crossed Nicols it presents
a dark base crowded with irregular patches of minute fibrous micro-
liths of a dull yellowish colour. (6) About an equal quantity of
roundish or irregularly polygonal grains of a pale yellowish green
mineral, which exhibits one marked set of cleavage-planes, and a
second less perfect at right angles; these, especially the former, are
further indicated by numerous grains and rods of opacite, probably
magnetite. With crossed Nicols this second constituent is either
black or shows a pale fibrous dull bluish mineral. The greatest
absorption takes place when the cleavage-planes are parallel to one
of the vibration-planes of the Nicols. (c) Scattered black grains and
erystals of magnetite or possibly chromite. No structure resembling
olivine occurs in the slide; so far as it 1s possible to conjecture the
nature of the unaltered rock, it most resembles one that has consisted
almost wholly either of two kinds of enstatite*, one richer than
the other in iron, or of enstatite and hypersthene. I much regret
that I could not succeed in finding the rock 7 situ.
The Ty-Ucha rock, on the contrary, has the granular structure
(defined by wavy irregular strings) which is often seen in an altered
olivine rock. These, with crossed Nicols, exhibit a slightly fibrous
structure and bluish-white colour, with an occasional golden-yellow
tint, aS is common in serpentines, the interstices being dark or
relieved by patches of dull bluish fibres. Opacite and larger grains,
generally rounded, but sometimes clearly crystals of the isometric
system, are scattered about the slide; probably these are magnetite.
No appreciable quantity of any other mineral is present in the slide.
This serpentine then probably results from the alteration of an olivine-
rock, a kind of dunite.
analyses:—I. is the dull-green chloritic rock, and II. the talcose schist.
No. L., however, has not made it easier to identify the chief mineral
it Ta
a “fC
eae Se Water’) Vane 286
Pe age oh SLO ee 56°34
50, ie eo NGOs. ai elieabe Deis 821
TOM es, 2-87 TNS ORy Oe Sees aoecr ct eechoe Ue
(Cie, Oe <RRbde pave en eea nee eee traces. ae % Rr Saas agg 2°00
isa C) ea een Te) OV terete yareeroeee neat ce, traces
ih Oo Je 1-73 Wa OE eRe Oe 0-52
MrOM 1579 Mg Oversees. 25°43
Gintepee 0-70 Na,O vieeeeeteeee eines 0°79
101-27 99-19
* Prof. Maskelyne has described an enstatite rock (without olivine or other
mineral, except perhaps diopside) from 8. Africa. Another slide cut from an
outcrop in this neighbourhood presents some resemblance to the above, though
the constituents are more minute and more highly altered, and there is less
iron.
A6 PROF. IT. G. BONNEY ON THE SERPENTINE
The Ty-Newydd rock* is similar to the last, but contains a little
of a mineral which, optically and in all other respects, resembles a
rather altered enstatite. One of the black grains shows a parallel
cleavage, as if it were a pseudomorph of enstatite in magnetite, a
thing not very uncommon in the case of augite. A few strings of
chrysotile traverse the slide.
The serpentine from Ceryg Moelion consists partly of a fibrous-
looking doubly refracting mineral akin to chrysotile, and partly of a
clear, rather satiny mineral, dark or faintly granulated with bluish
light, resembling one of thoso described in the block found at
Cruglas (a), with thickly clotted opacite in irregular strings and
some scattered grains. It may be an altered olivine rock.
The rock from a small quarry about a quarter of a mile north of
Plas Goch appears to be mainly composed of flaky mica-like plates
of a doubly refracting serpentinous mineral, with the usual granules,
rods, and clotted strings, probably of magnetite, and a very little of
the mineral described above (5) in the block found at Cruglas. Of
all those examined, it most resembles an altered olivine rock.
A slide cut from the tougher serpentine in the quarry south of
Cruglas shows a rather peculiar structure. The slide is traversed by
irregular strings of clotted opacite, and is composed of two closely
associated minerals—one the scaly serpentine described above, the
other exceedingly minute scales of a doubly refracting mineral,
dichroic, changing from pale yellowish to dull grey-brown, and with
the two Nicols giving fairly brilliant colours. There is nothing
inconsistent with “this serpentine being the result of the alteration of
an olivine rock; but, so far as my experience goes, its appearance is
exceptional. As stated above, I could see no evidence that this
variety was intrusive in the normal serpentine.
Microscopic examination confirms the view taken in the field, that
several of the so-called serpentines are true gabbros. The specimen
from the great mass near Ty Newydd shows the ordinary structure
of a typical gabbro, though the felspathic constituent is wholly re-
placed by secondary products (much being an opaque dust), being
thus a variety of the saussuritic mineral so common in old gabbros.
There is also plenty of a rather coarsely cleaved diallage, with pro-
bably some ordinary augite, and a few grains of a more finely
* JT am indebted for the following analysis of this ser penline to the kindness
of B. T. 8. Houghton, Hsq., F.G.S. :—
Wrater! 2120.0 ge nase decsaeeceae nee enanee 12°52
No) is © RPA ACA as ioseubhencindn condoan wan udsoooo: 3862
v0 O SR REPREP POM! isn cn nen Ut ane isco Qhudbccaences 415
NCE 0 Riper eres eres Séscadeedoe bol Dicer 5:21
1D @ MORENO Re SUNG Nobo cd oor hyedbedonansate 4°34
VEO) Se con «cade ae One e nere Seee traces.
OL 0 RRR AEs See orice ad uoasa)scuondosbuon co traces.
A Fa 0 ERP RRM REN Ce Chadonscbancdnas an sacsoc 33°83
Faull. <0 (21: Speen eR eREM iE Moca aciquhaaanuoraocdsac 0-70
AND ASSOCIATED ROCKS OF ANGLESEY. AT
cleaved fibrous mineral of an altered aspect. This may be only
the result of pseudomorphic action on the diallage; but it may have
been from the first a separate mineral. I incline to the latter view,
as the normal constituent is sometimes altered, but seems then to
produce a different mineral.
A specimen from the islet near the south shore closely resembles
the last. Here the pyroxenic mineral sometimes contains microliths,
apparently of augite, sometimes exhibits lamellar twinning ; it is
occasionally altered as in the last case. A third specimen, from a
knoll on the shore between an outcrop of schist and another of ser-
pentine, corresponds generally with the above.
Specimens of the normal schist from near the chapel on the Holy-
head island, from near Tycoch, and within about 5 feet of the ser-
pentine at the presumed intrusive junction (see above, fig. 1, p. 41)
have been examined. They are representatives of a class of schist
of which I have seen and received numerous examples from Anglesey.
Under the microscope they are seen to be composed mainly of two
minerals, both of minute size:—one quartz; the other a greenish
mineral in little scales*, fairly dichroic, changing from a greenish
yellow to a strong green, occurring also in veins in little tufts:
it resembles a chlorite more than a mica. There is an occasional
granule of epidote and a good deal of a sort of grey earthy dust,
sometimes in clots, probably in part decomposed magnetite or ilme-
nite. There are also some yein-like bands of clear quartz, probably
segregation-products. The third specimen has a rather coarser
structure, and contains some scattered quartaz-grains which may
indicate original constituents. These rocks show a banded structure,
probably due to original bedding; but they are very highly altered.
The schistose rock at Tyddyn Gob, as might be supposed from its
aspect, is very different. It has a marked. foliated structure, being
chiefly composed of wavy bands of an earthy mineral, almost opaque,
and of a at colourless fibrous mineral, probably a variety of
actinolite. Among the latter, in the lower and coarser rock, are
the remains of a mineral with well marked parallel cleavage, from
which the other may have been produced by secondary change. In
appearance the mincral more resembles augite, and it is practically
not dichroic; but in other optical properties it agrees better with
hornblende; a little epidote is present. I cannot help suspecting
the possibility of this rock being an altered gabbro with pressure
foliation ; but if so, it is a most exceptional ease.
From the above observations it will appear that the whole of this
district needs remapping; and this task will not be an easy one.
That the gabbro is an ordinary igneous rock cannot, I think, be
doubted. “AS regards the serpentine, the evidence is a little less
clear. The microscopic structure, owing probably to the great age
of the rock, is rather obscure and anomalous ; its relations to the
schist are not clearly displayed. Still the structure in several cases
coincides with that of serpentines which we need not hesitate to
* Not more than ‘001 inch diameter.
A8 PROF. T. G. BONNEY ON THE SO-CALLED
consider altered olivine rocks, such as those of Cornwall, Scotland,
Italy, &c.; the general aspect of the rock in the field perfectly agrees
with the same; and its relation to the schist would be most difficult
to explain, except on the theory that it was intrusive in the latter.
We must also remember that olivine rock partially altered has been
detected in the Lleyn peninsula*. The evidence in favour of the
serpentine being produced from the schist by some kind of selective
or local metamorphism is of the weakest possible description. We
therefore need not hesitate to add the Anglesey serpentines to the
list of altered peridotites.
2, THE SO-CALLED SERPENTINE OF PoRTHDINLLEYN.
The northern and larger part of the promontory at Porthdinlleyn
(west of Nevin) is coloured as serpentine in the Survey map, and
thus noticed (by Mr. Selwyn) in the memoiry :—‘“* The rock at Porth-
dinlleyn is a kind of coarse green and purple serpentine, with nests
of red jasper ; veins of the serpentine are observed to dash in among
the slaty series at Porthween.” So far as true serpentine is con-
cerned, [ might have modelled this note on the well-known chapter
concerning the snakes in Iceland; for there is none at Porthdinlleyn.
The rocks, however, which I examined in my search for serpentine
are so interesting that I am tempted to add a few words concerning
them.
Specimens of several of these rocks have been examined microsco-
pically ; and one or two exhibit structures of much interest. On the
present occasion, however, I shall not enter into details foreign to
the immediate,subject, but only endeavour to identify the specimens.
The first rock seen (by a landing-stage) as we approached Porth-
dinlleyn along the shore from Bwlchdinlleyn is a massive green rock
of serpentinous aspect. In the craglets and reefs near the hamlet
itself we find a similar rock which also shows in parts a distinctly
brecciated structure, pale-green fragments of various sizes (generally
up to 2 or 3 inches diameter, but in one case about 18 inches)
occurring in a darker and more ashy-looking matrix. In other
parts the structure more resembles brecciation in situ ; sometimes
the rock is almost spheroidal, and reminded me of certain instances
which I have seen in old igneous rocks of a rather basic nature, where
the outer shells of the spheroid had become decomposed, simulating
a conglomerate with but little matrix. A reddish variety of the
compact rock also occurs ; and these rocks continue for some distance
to the north of Porthdinlleyn, the “ nests of red jasper ” (hematite
with quartz, calcite, &c.) being in places very conspicuous. In the
field it is very difficult to pronounce upon the nature of the above
compact rock. It is hard, with a subconchoidal to rather argil-
laceous fracture, traversed by well-marked divisional planes, but
«x Geol. Mag. dee. ii. vol. vii. p. 208.
t The Geology of North Wales, p. 170.
SERPENTINE OF PORTHDINLLEYN. 49
with no certain indications of bedding. The rock exhibits spots of
epidote, varies in colour from a dull sap-green to a greenish-purple
colour, is traversed by thin veins of quartz and calcite, and
might be taken either for a compact chloritic rock resulting from the
alteration of a uniform fine sediment, or for a very compact diabase.
Under the microscope both varieties are seen to be rather decom-
posed, the slides being rendered more or less opaque with fine
powdery ferrite, which sometimes also occurs in granules. There
are indications of numerous microliths, some doubtless being felspar,
and probably a plagioclase ; these, in places, show a tufted, sometimes
an almost spherulitic arrangement. In this are scattered some
larger augite crystals, much altered but still recognizable. The
green variety has some faint indications of a fragmental structure,
and might be a tuff in which the outlines of the fragments were
nearly obliterated. The structure of the redder variety is more
distinctly that of a true igneous rock; and as I could see no signs of
a division in the field, we may venture to identify these as compact
diabases*, very probably old flows of a basaltic lavat. The breccia
exhibits under the microscope a base of filmy pale-coloured viridite,
in which are scattered numerous granules of ferrite, crystals of
epidote, with other minerals of secondary formation, altered augite,
and felspar, and scattered fragments, apparently of more or less
glassy lapili. Of the nature of some of the last there can be no |
doubt. The rock, then, is a ‘“diabase tuff,” of which probably a
good deal was once a very fine dust.
For some distance to the north of Porthdinlleyn the dubiously
“‘ conglomeratic ” aspect of the rock as above described continues ;
and then we find, on arriving within a short distance of the life-
boat house, sections that, even in the field, are perfectly conclusive.
The best occurs in a little cliff (an old quarry-face) looking seaward.
On the sides of this (the section is about a dozen yards wide) we
find a dull-green ashy-looking matrix, full of angular and subangular
fragments of all sizes up to 3 or 4 inches diameter of a compact
paler-coloured rock; and in the middle a mass of rounded blocks (a
foot or two in diameter) which seems almost solid passes irregularly,
but with fairly marked boundaries, into breccia. There can, then, be
no doubt that we have here a true volcanic agglomerate, including
either a thickly fallen mass of bombs or a small lava cowlée. This
view is fully confirmed by microscopic examination,—the breccia
exhibiting a ground-mass, as above described, full of scattered frag-
ments obviously of volcanic origin, some & brown slaggy glass, like
a, kind of tachylite, others compact basaltic scoria. The examination
of a spheroidal mass from the agglomerate shows it to be highly de-
composed compact diabase.
* The name diabase is given, though little or no chlorite can be recognized,
because I know of none other that exists.
t+ I may mention that I have in my collection a rock microscopically identical
with the above, which I collected between Glyn Garth and Beaumaris. ‘These
old basalts are, i suspect, not uncommon among the Welsh Pre-Cambrians, and
in the field are hard to recognize.
Q. J.G.S. No. 145. E
50 PROF. T, G. BONNEY ON THE SERPENTINE
Proceeding a little further, we find, about fifty yards south of the
boathouse, a compact green rock with indubitable spheroidal strue-
ture. This rock now continues along the northern and western face
of the peninsula, becoming in places very distinctly spheroidal. The
face of a crag (a joint-plane) near the sea at the N.H. angle exhibits
one of the most conspicuous instances of the structure that I have
ever seen. The rock, where not spheroidal, is compact and sharply
jointed, in one or two cases a little platy in structure. Under the
microscope it is seen to be an altered basalt, the structure being
recognizable, though the felspar is replaced by earthy decomposition-
products, and the grains and crystals of augite are much altered.
1 also noticed one or two small dykes, seemingly of late date. The
eastern side of the peninsula had occupied so much of my time that IT
was unable to examine into the relations of the above group of rocks
with the schist of the district (which is not to be seen on that side),
and had to be content with satisfying myself that, though there are
igneous rocks, there is no true serpentine at Porthdinlleyn.
Discussron.
Mr. Baverman had examined the steatite-deposit of the locality,
and had arrived at much the same conclusions as the author.
There were true serpentine rocks, and doubtful or “‘ serpentinous ”
ones. He considered an examination of the composition of these
rocks desirable.
Dr. Hicks congratulated the author on speaking of the mtrusive
origin of the Anglesey serpentines with a certain degree of doubt.
He was himself inclined to regard these rocks not as intrusive, but
as altered representatives of certain ancient sediments. He repudi-
ated the notion of “ selective metamorphism ” being generally ap-
plicable to these rocks. The rocks at Porth Dunbar he regarded
as mainly indurated and altered ashes.
Prof. Huenrs pointed out that when the Survey map was made
the definition of “serpentine” was much wider than that which
was now adopted. He was not convinced of the intrusive cha-
racter of the serpentines in the section given by the author, but
thought it might be one of the numerous cases in which during
the crumpling of the gnarled series the harder masses were pro-
truded through the schists, producing small local faults. He believed
that calcareous beds in the gnarled series, and magnesian minerals
in the dykes, generally associated with the serpentinous rock and
ophicalcite, were sufficient to account for both.
Mr. Hupirston had examined the rocks of the district, and
thought they differed so greatly from the Cornish serpentines as to
make it somewhat doubtful whether they could have been formed
by the alteration of olivine rocks of intrusive origin. He was in-
clined to think that the Anglesey serpentines, like those of the
Shetlands described by Dr. Heddle, might in part be altered acti-
nolitic rocks,
AND ASSOCIATED ROCKS OF ANGLESEY. sy |
The Avrnor doubted whether the so-called steatite is really the
normal mineral. Dr. Hicks had entirely misapprehended him ; for
he had no doubt that the true serpentines of the district were
altered olivine rocks, and not metamorphosed schists. He con-
sidered the use of the term “ serpentine” by the Survey, if it were
as stated by Prof. Hughes (which he doubted), was one which was
quite unjustifiable ; nor could he agree with Prof. Hughes’s expla-
nation of the section showing an apparent intrusion of the serpentine
into the schist. He could not admit that either the Anglesey ser-
pentines or any Scottish serpentines which he had himself examined
could have been formed by the alteration of actinolitic rocks.
5y4 PROF. SEELEY ON A SMALL LIZARD FROM THE
5. On Remains of a Smart Lizarp from the Neocomian Rocxs of
Comin, near Trreste, preserved in the GrotogicaL Musgun of the
University of Vienna. By Prof. Srxrny, F.R.S., F.G.S8., of
King’s College, London. (Read December 1, 1880.)
[Puars IV.]
Prorrssorn Epuarp Svzss, F.M.G.8., recently received from Comén,
near Trieste, a specimen showing the hinder half of the skeleton of
a lizard which he has desired me to describe. Unlike the two fine
slabs from the island of Lesina, preserved in the k.-k. geologische
Reichsanstalt, which are in a pale yellowish limestone matrix,
this specimen is from a limestone slab nearly black; the animal
shown upon it has lain exposed for some time in the quarry and
suffered by the solvent action of the rain. Prof. Suess mentioned
to me that the colour merely indicated one of the many alterations
in the limestone, and that, since it was collected by a former pupil,
no doubt could attach either to its stratigraphical or geographical
position. Prof. Kornhuber does not appear to have been quite cer-
tain as to the position of the Lesina rocks in the Cretaceous series ;
but while [ was in Vienna, Professor Pisani mentioned to me that
he had identified thirteen species of fish with Upper Neocomian
species ; and as fish constitute the chief fossils of the deposit, this
must be held conclusive evidence of the geological age of these
lizards.
This new fossil (PI. IV. fig. 1) at first sight presents a considerable
resemblance to the Hydrosaurus lesinensis of Kornhuber, as was
pointed out to me by Prof. Suess; but the differences are so
remarkable and important that I find myself unable to inelude it in
the same genus. The specimens in the Museum of the Imperial
Geological Survey were shown to me by the Director Franz Ritter
von Hauer. They are admirably preserved, and, as Koruhuber has
stated, appear to indicate an animal with 9 cervical, 30 dorsal, and
2 sacral vertebrae, and a tail of which only the 24 anterior vertebre
are preserved. The type 1s distinguished by the remarkable stoutness
of the dorsal ribs, by the very long and large neural spines and early
caudal vertebrae; and it possessed | well-developed limbs, of which the
hinder pair were much larger than the anterior pair. The specimen
which I have now to describe has only the hindermost 12 dorsal
vertebre preserved. There are presumably 2 sacral vertebre ; and
then succeeds the tail, of which about 65 vertebra are preserved
or indicated by impressions ; and it is probable that more remained
in the slab which had been adjacent but was not collected.
The length of the 12 dorsal vertebra is about 55 millims.; and
the remainder of the vertebral column, as preserved, measures along
the curves of the tail nearly 200 millims. The dorsal region is ex-
posed so as to display the attachment of the ribs. The ilium is the
Quart. Journ. Geol. Soc. Vol. XXXVIL.PL IV.
ST
tf)
g
re
A.S.Foord del. et lith. dias Mintern Bros. mp.
ADRIOSAURUS SUESSII.
NEOCOMIAN ROCKS OF COMEN, NEAR TRIESTE. D3
only pelvic element clearly exhibited; and that is directed backward in
the usual lacertian manner (fig. 1,1). The hind limbs are preserved,
though they were fast becoming obliterated by weathering. The caudal
vertebrve lie upon one side, and consequently do not give a very dis-
tinct idea of their forms. They, however, show no trace whatever
of the neural spine, though the chevron bones are well developed,
and are preserved down the greater part of the tail. The dorsal
vertebrae apparently rest upon the neural surface and expose the
visceral surface. This may be inferred from the form of the cen-
trum, the curvature of the ribs, which are concave in length as
exposed, and the fact that the ilinm underlies the femur; but the
face of each centrum has been somewhat dissolved, so that 1b cannot
in any ease be said to exhibit the unaltered appearance of the bones.
Each centrum in the dorsal region is rather less than 3 a centim.
in length, and is about 6 millims. widein front. The sides converge
posteriorly to about 3 millims. ; so that, besides being a far smaller
animal, the lower dorsal vertebree appear here to be relatively
shorter, and the centrum, instead of having the concave lateral
outlines of Hydrosawrus, has its side rather convex in length;
and the anterior surfaces on each side of the anterior articulation
look more forward and less outward than in that genus. There
1s, moreover, no indication of the transversely concave outline of
the intervertebral union—but in place of it a notch in the ante-
rior border, as though there were a small ossicle at the junction of
each two vertebre; but this apparent notch may be nothing but
the neural canal exposed in this position by the thin base of the
centrum being there dissolved. As the vertebree pass downward
towards the sacrum, their aspect seems to be less massive, and the
posterior end becomes a little more compressed from side to side.
There are slight indications of two ridges running longitudinally
on the base of the centrum from the outer corners of the anterior
cup towards the posterior articular ball. All the dorsal vertebree
were furnished with ribs; but they become shorter and smaller
towards the sacrum. On the right side of the specimen they lie
together, touching each other along their lengths, except in the case
of the last three or four, which are only indicated by impressions.
The ribs appear to be flat on the under side and moderately curved ;
the rib of the third vertebra preserved is 2 centims. long and 2
millims. wide at the proximal end. The ribs appear to be tubular
and single-headed; they taper evenly to a blunt point, but scarcely
give the impression of being relatively so stout as the ribs of Hydro-
saurus. The sacral vertebra are no better defined than those of the
dorsal region, being partly covered by femoral bones. ‘There is an
angular bend in the tail, beyond which the vertebre le on their
sides more perfectly displayed than in the case of the first few caudals.
The neural arches of the caudal vertebre were low, without any indi-
cation of neural spines, the neural arch being concave superiorly from
front to back, and articulating with the arches of adjacent vertebre
by zygapophyses, which were elevated high above the neural sur-
face. The neural arch widens in front, and is smooth at the sides.
ot PROF. SEELEY ON A SMALL LIZARD FROM THE
There is no trace preserved of transverse processes, such as may be
presumed to have existed. The chevron bones are relatively long and
slender and directed backward parallel to each other. The vertebrae
rapidly decrease in size, and in the latter half of the tail preserved
are small. These hindermost vertebre (that is, after about the
thirty-fifth) appear to develop a slight neura: spine, which is slender,
directed backwards nearly horizontally, and terminates without any
decrease in thickness, in a rounded end; but these spines can only
be detected in some eight vertebra. The neural arch appears to be
preserved to the end of the series, where the whole lateral measure-
ment of the vertebra is less than 2 millims., and its length does not
ereatly exceed 2 milims. The height from the base of the centrum
to the middle of the neural arch at about the eighth caudal is 34
millims., the neural arch forming less than half of this height. The
union between the centrums is not well defined. The chevron bones
in the first dozen vertebre appear to be about 53 millims. long.
There thus appear in the tail to be differences from Hydrosaurus
desinensis in the relatively small development of the neural spine,
which never extends upward as a broad plate in this form, and,
when it does exist, is a slender backwardly-directed process. The
earlier chevron bones in the present fossil appear to have been rela-
tively broader; and in the absence of any indication of transverse
processes, it is impossible to affirm that those processes existed.
The pelvis is imperfectly seen on both sides. The ilium extends on
the right side parallel to the vertebree (fig. 1, 1), but its anterior part
is covered by the head of the femur. The part exposed is fully 7
millims. long; its outer edge is rounded; it expands anteriorly a
little, but appears to be distinguished by its slender form and parallel
sides. On the left side of the specimen, underlying the other femur
and articulating with a bone in front, which may well be the arti-
cular part of the ilium, is a curved bony element (nearly 8 millims.
long, wider than the ilium), which from its position might well be
the ischium. ‘The bend in it occursin its anterior third ; 1t is com-
paratively slender, and only expands a little at its distal end. The
slender form of the ilium and its relative length are points of differ-
ence from the species with which this has been compared. Both hind
limbs are fairly well preserved. The femur of the left side (fig. 1, m)
is about 11 millims. long, a good deal constricted in the middle, and
flattened and expanded at the distal end, which is concave from side
to side; the anterior margin of the bone is concave in length, while
the posterior margin is more straight. The characters of the arti-
cular head are not well defined, owing to the way in which the bone
is compressed; but the head appears to have been well rounded, and
to have measured about half a centim. from front to back. There
are no indications of the distal epiphyses represented by Kornhuber.
The tibia (fig. 2, ¢) has its anterior margin straight, and its pos-
terior margin concave. It is about 7 millims. long. The proximal
end is greatly expanded; and the shaft is relatively more slender than
in Kornhuber’s species. The fibula (fig. 2, f) is a rather more slender
bone, without any indication of proximal expansion ; it widens at
NEOCOMIAN ROCKS OF COMEN, NEAR TRIESTE. 55
the distal end to 3 millims., which about corresponds to the proximal
width of the tibia. The tarsal bones (fig. 2, ts) are not well preserved,
but appear to consist of one large bone below the tibia, which is appa-
rently polygonal, and two smaller bones placed below the fibula; but
there has probably been at least a third bone, which was distal in
position and is not preserved. The metatarsus (fig. 2, mt) is not very
distinct ; and it is difficult to say whether the metatarsal bones were
entirely distinct from each other. The specimen would appear to
indicate that there were at least three metatarsals. The bone
below the large tarsal element is short and broad, reminding one in its
proportions of that of a Plesiosaur. It articulates by a large proximal
facet with the large tarsal bone, and by a small facet at the proximal
end with the distal tarsal element adjacent to it. Its width at the
proximal end is over 2 millims.; and it appears to be about 4 millims.
long. The metatarsals on the outer side are not preserved. There are
five digits (fig. 2,1-v) formed of slender bones with a median groove
on the dorsal surface of the first row. There are two bones in the first
digit, which is short and terminates in a pointed bone, the distal end of
which is a little curved and apparently carried a claw. There are
three bones in the second digit, which is about twice the length;
but the fracture in the slab passes through the middle of the ter-
minal small phalange. In the third digit there may have been four
phalanges; but the fracture passes through the third, which is so
large that it is not likely to have carried a claw. There appear to
have been four phalanges in the fourth digit; and in the fifth the
number cannot be satisfactorily determined ; but there do not appear
to haye been more than three. The three inner digits have the
proximal surfaces of the proximal row of bones in the same line ;
but the two outer digits look as though placed a little higher up,
which is in accord with the ordinary Lizard plan. The totallength
of the longest digit as preserved is about 9 millims.; and the total
length from the proximal end of the tibia is a little over 21 millims.
It will thus be seen that the tarsus and digits differ considerably
from those indicated by the animal described as Hydrosawrus lesi-
nensis.
It is of course with this type that the present specimen must be
chiefly compared; and the form and proportion of the dorsal ver-
tebree, the mode of articulation of the ribs, and the characters of the
caudal vertebrae, especially in the neural spine and transverse pro-
cess, indicate a distinct type. The pelvis is also distinct, while the
proportions of the segments of the limb differ in as remarkable a
way, and necessitate placing this fossilin a distinct genus. Though,
from the imperfect preservation of the specimen, its more important
characters remain unknown, it may be conveniently distinguished
as Adriosauwrus Suessit. Its affinities need the assistance of more
perfect remains for their elaboration.
I am indebted to Prof. Suess for the opportunity of making this
ecord, and adding another species to the Secondary representatives
f the lizard group.
56 ON A SMALL LIZARD FROM THE NECOMIAN ROCKS.
EXPLANATION OF PLATE IV.
Fig. 1. Tail of Adriosawrus Suessit, natural size: 1, ilium; m, femur.
2. Hind limb, from right side, enlarged: 7¢, tibia; f, fibula; ¢s, tarsus ;
mt, metatarsus ; I, I, Il, Iv, V, digits. ;
Discussion.
Mr. Huzxe said that he had no doubt that the species described
by Prof. Seeley belongs to a genus distinct from Hydrosaurus. He
compared the former with the Geckos in respect of their having
bony scales.
The Avurnor stated that the distinction of the vertebrae had been
rendered difficult through chemical action. He doubted as to the
existence of scutes in the specimen.
AMMONITES FROM THE INFERIOR OOLITH. oi
6. On the Terminations of some Ammonites from the Inrertor
Oorrre of Dorser and Somerset. By James Buckman, Hsq.,
E.G.S., F.L.S., &e. (Read June 23, 1880.)
Durine the progress through the press of D’Orbigny’s ‘ Palconto-
logie Francaise, ‘‘ Terrains Jurassiques,” I was busily engaged in col-
lecting the fossils of the Inferior Oolite and Lias in the neighbour-
hood of Cheltenham. In both of these rocks I had the good fortune
to find a somewhat large series of Ammonites, the greater propor-
tion of which I could readily identify from D’Orbigny’s figures*.
But as these fossils were in bad condition, especially when com-
pared with the French drawings, I was at first almost led to think
that these latter had been somewhat unjustifiably made up or, as
we should say in plain English, “ fudged.”
Thus, in reckoning up the plates of admitted Inferior Oolite Am-
monites in the ‘ Paléontologie Francaise,’ we find them to be thirty-
eight, out of which no less than twenty species (a httle over two
thirds of the list) are drawn with the mouth of their shells more
or less perfect; and yet, strange to say, I do not recollect a single
example of their Cotteswold prototypes having occurred to me in
this perfect condition.
Since those days of scepticism, however, D’Orbigny’s book has
become my constant and trusted companion, as the specimens in
our Dorsetshire list of Ammonites appear to be in much the same
condition as those figured by that talented author.
During the last seventeen years my lot has been cast in the
pleasant county of Dorset; and, curiously enough, the farm that I
haye occupied is situate on the Inferior Oolite ; the Halfway-house
quarry is within a mile of my own residence; whilst a quarry in
one of my own fields, within a hundred yards of my house, has
proved to be one of the richest in England, if not in the world, in
Oolitic fossils, and especially in the species of the Cephalopoda
and Gasteropoda, in each of which great classes we may safely
reckon as many as from sixty to seventy species. From this quarry
and the surrounding district, there haye been determined as many
as twenty-eight species of Brachiopoda; and I probably possess
nearly, if not quite, a hundred forms of Lamellibranchiata, which,
not to name other remains, cannot but be considered as a goodly
list.
If, again, we consider that the greater part of the individuals of
these lists occur in a bed varying from 2 to 3 feet in thickness,
the surprise becomes still greater ; and net only are the species so
numerous, but it is one mass of specimens, as, instead of our merely
finding an Ammonite here and there (as in the Cotteswolds), this par-
ticular bed is a mass of them, so that several species will be huddled
together in a small space; and, in so far as the Ammonites are
* The part on the ‘‘ Céphalopodes” was finished in 1849.
58 J. BUCKMAN ON AMMONITES FROM THE
concerned, on the same slab will be representatives of several of the
zonal divisions of different authors. This may be judged from the
fact that on the surface of slabs from this bed other Ammonites
besides the following have been noted.
Ammonites jurensis, Zev. Ammonites Gervillii, Sow.
—— Sowerbyi, Miller. —— Brongniarti, Sow.
—— Humphriesianus, Sow. —— subradiatus, Sow.
—— Braikenridgii, Sow, —— leviuseulus, Sow.
—_— linguiferus, D’ Orb. —— discus, Sow.
—— Sauzei, D Ord. —— Parkinsoni, Sow.
Some species prevail to such an extent that hundreds of indivi-
duals may be found in a square yard of the bed, one species prevail-
ing at one quarry, and another at other quarries.
So numerous are individuals in some quarries, and so varied do
they seem, that it is hardly possible to escape the conclusion that the
family must have hybridized to a considerable extent. Anyhow,
under such circumstances, it is exceedingly difficult to accurately
define species—much more so than in the Cotteswold district, where
it would be difficult to find more than half a dozen forms in a
day.
But besides this, when we compare the Dorset and Somerset Am-
monites with the Gloucestershire forms, we find that the former
are usually sharp and well preserved, while the latter are consider-
ably rougher and more fragmentary. Thus it is that shells with
their terminations are rare in the latter county, while with us they
are comparatively common.
The specimens laid before the Society are a sufficient evidence of
this fact; and they are fast increasing, now that this matter is being
more carefully investigated, the truth being that collectors seem to
have vied with each other in squaring up the mouths to make them
neat and tidy. Many among them, indeed, would cut away ald of
the outer chamber, preserving only the inner chambers, which, being
more or less filled up with carbonate of lime, were said to be alive,
whilst the outer one, filled up with indurated mud, was pronounced
to be dead, and so was removed as useless.
But not only do we find our Dorset specimens to be much like
the French ones (as figured by D’Orbigny) in condition and state of
preservation, but the species from the two sides of the Channel are
almost identical: thus we have within jour of the whole of D’Or-
bigny’s figured specimens from the Inferior Oolite of France.
But, besides this, there are several species in our own Cephalopoda-
bed, now admitted to be high up in the Inferior Oolite, which
D’Orbigny has allocated to the Lias. This, we take it, has been
mainly due to the fact that this bed has been confounded with the
ene at the base of the Inferior Oolite in Gloucestershire.
In this list are the following :—
Ammonites insignis, Schiidl, Ammonites Germaini, D’ Orb.
—— variabilis, D Ord. —— jurensis, Zict.
—— Murchisone (?), Sow. —— cornucopia, Young § Bird.
—— discoides, Ziet. —— torulosus, Schiidl.
INFERIOR OOLITE OF DORSET AND SOMERSET. og
Now as to the forms which up to this time we have found with
terminations to their shells, we may state that as yet we have only
met with fourteen; but it happens, as a rule, that the species so dis-
tinguished number several individuals, though some three or four
of them have only yielded single specimens.
Our list, then, includes the following species :—
Terminations.
. Ammonites concavus, Sow.
. -—— subradiatus, Sow.
—-- Kdouardianus, D’ Orb.
—— Braikenridgii, Sow.
—— linguiferus, D’ Orb.
—— Sauzei, D’ Orb,
—— Martinsii, D’ Ord.
-—— subcostatus, Buckman, MS.
—— Gervillu, Sow.
—— Brongniarti, Sow.
—— Manselii, Buchman.
. --— Humphriesianus, Sow.
Moorei, Lycett.
. —— boscensis, Legnés.
Lanceolate ...... J
Ovate-lanceolate
or spathulate.
semicircular.
WWieivedes focal. :
HA Oo NYS oO OO I TB Go BO
l
\
Delphinulate, |
|
Here, then, we have given fourteen species of Ammonites with
their terminations more or less complete ; and for these we have at-
tempted to make a provisional classification.
So far as we have been enabled to examine these more complete
Specimens of Ammonites, we arrive at the conclusion that, the
terminations to the shells are capable of greatly aiding in the
determining of species, as trimmed-up examples of A. linguiferus,
with their broadly oval or spathulate mouths, are difficult to distin-
guish from A. Humphriesianus ; but when we have the semicircular
rugose mouth of the latter for comparison with the former the
difficulty vanishes. Thus, again, the lanceolate termination of the
discoid A. subradiatus is very different from the spathulate or ovato-
lanceolate ending of A. subcostatus (Buckm.); and yet these two forms
have been referred to one species by different authors.
The dephinulate mouth in A. Gervilliz is a complicated ter-
mination when compared with the plainer semicircular terminations
of A. Brongmarti and A. Humphriesianus ; and yet without this
knowledge we had always confounded the first two forms.
From these remarks it seems but reasonable to conclude that the
terminations of Ammonites may become important in the distinguish-
ing of species, though, from what we have seen, their preservation is
of somewhat rare occurrence; at the same time our own experience
seems to point to the fact that many fine examples of more com-
plete shells have been lost from the want of due observation upon
the subject. We may further mention that, with the vast numbers
of Cephalopada which are everywhere around us and which are so
perfect in other respects, we have not yet seen a single example either
of Rhyncholites or Trigonellites. Mr.S. P. Woodward, however, has
figured an Ammonite with the operculum from Dundry*. The shell
* See ‘ Geologist, vol. iti. p. 328.
60 J. BUCKMAN ON AMMONITES FROM THE
is referred to A. subradiatus ; but it is very different from that which
is now recognized by this name,—A. Brightii, which it is said to
resemble, being an Oxford-Clay fossil, while the Dundry Oolite is
the exact equivalent of the Dorset Cephalopoda-bed. I hope there-
fore some day to see this specimen in its place at the British Mu-
seum.
I now proceed to pen a few notes on these fourteen forms which
we have observed to present more or less perfect terminations to
their shells; and in doing so I would express the hope that ere
long other forms will be met with to enable us more clearly to un-
derstand the value of a more complete structure, while at the
same time it may not be too much to express a hope that better
specimens may yet be found than those we already possess or,
through the kindness of friends, have had access to.
Nores ON THE SPECIES.
Fig. 1.—Termination of Ammonites concavus, Sow.
Toe S
WWM
SA
1. AmnmonrTEs concavus, Sowerby, pl. 94, fig. 2. (Fig. 1.)
This is a very common shell in the Cephalopoda-bed in Dorset
and Somersetshire, occurring less frequently in the same horizon in
Gloucestershire. It is a very variable shell; and hence its syno-
nyms are unusually numerous. |
In this district we have usually named it A. subradiatus; and it is
here only retained because A. concavus was figured by Sowerby from
a specimen obtained from this neighourhood.
INFERIOR OOLITE OF DORSEY AND SOMERSET. GL
Fig. 2.—Termination of Ammonites subradiatus, Sow.
SS
Z)
Ze)
2. A. suprapiatus, Sow. pl. 421. fig. 2; D’Orb. pl. 118. fig. 3 (now
ie 2); also D’Orb. pl. 129. fig. 3.. (Fig. 2.)
The difference insisted upon seems to be that in A. concavus the
curved radii are seldom branched, whilst in A. subradiatus, the
radii are either branched or have short intermediate ones between
the longer ones. There is, however, so much variation in this
respect that we still hold these to be mere varieties.
We have now several complete examples of the termination ; but
the first specimen was obtained by Captain Kennedy from our own
quarry so perfect that it might have sat for the portrait given by
D’Orbigny, pl. 129. fig. 3. It is a very common fossil, and in
some quarries occurs mixed with the former so thickly that hun-
dreds of examples could be got ina day ; and yet a specimen with even
the base of the termination 1s very rare.
3. A. Epovarpianus, D’Orb. pl. 130. figs. 3-5.
Is found sparingly with the examples just quoted. Our two
specimens are the only ones we have meth wit in the Bradford-
Abbas quarry ; and, curiously enough, they have both indications
of the termination.
4, A. Brarkenripert, Sow. Min. Conch. t. 184. (Fig/3.)
This shell was figured by Sowerby in the second volume of Min.
Conch., which bears date 1818 ; the specimen, a very imperfect one,
was from Dundry, near Bristol. In his description he has the fol-
lowing remarks* :—
“Perfect terminations of the Ammonites are scarce. I have,
however, met with several specimens indicating the form of the lip;
but none of them exhibit much out of the usual way, excepting
some French ones and those now before us: in one of the French
specimens the aperture is much contracted by the lip; in another
the lip forms a single arched lobe slightly bent inwards.”
* Min. Conch. vol. ii. p. 187.
62 J. BUCKMAN ON AMMONITES FROM THE
Fig. 3.—Ternunation of Ammonites Braikenridgii, Sow.
SY
yA
a. Krom the side. 6, From the front.
Our Cephalopoda-bed is on the same horizon as the bed from
which the Ammonite just quoted was obtained, Dundry being the
extreme western extension of the Oolitic system which prevails in
Dorset and Somerset, which latter has so much resemblance, as evi-
denced by fossils, to the Inferior Oolite of France.
This fossil is usually found most abundantly at Clatcombe, near
Sherborne, where examples with the curious terminations are not
uncommon; and it illustrates one of those cases in which a different
species of the genus occurs at one quarry from that which prevails
at another. It is occasionally found at Bradford Abbas, where the;
prevailing Ammonites are A. concavus and A. Sowerbyt.
The terminations in this species are among the most perfect, as
well as the most frequently met with. The spathulate projection
varies greatly both as to length and breadth.
5, A. trincurrerus, D’Orb. pl. 136. figs. 1 & 2.
Has a neat form and a less broad spathulate termination than the
preceding, though closing up the aperture of the shell more by
reason of its bending inwards. It is thinner in the whorls; and
the ribs are in threes at the back of the shell, uniting into one, with
a tubercle in front. Sometimes there is an intermediate rib between
a pair, with three-ribbed vaultings.
This shell is by no means so frequent as A. Braikenridgu, but
occurs in the same places, intermixed with it.
6. A. Savzer, D’Orb. pl. 139. figs. 1-3.
The termination of this shell is much like the former; but its
ribs are much larger, and the shell broader. It is also inclined to be
unsymmetrical, and has but few whorls.
INFERIOR OOLITE OF DORSET AND SOMERSET. 63
This is not uncommon with the termination both near Sherborne
and at Bradford Abbas.
These three last species are admirably figured by D’Orbigny ; and
yet we are happy to think that our Dorset examples are quite up
to the perfection of the French ones.
fake Martins, D’Orb. pl. 125. figs. 1, 2.
Ts not uncommon; but the small specimen we have seni is the
only case in which we have observed the terminal Jip. It seems to
have been the first lip formed; and if fig. 3 of D’Orbigny’s plate
represents the lip of an older specimen, it would tend to show that
the lips vary very much with age. Our specimen is from Bradford,
where the species is not uncommon.
gs. A. suscostatus, Buckman, MS.
This shell, from near Sherborne, belongs to the discoid section of
Ammonites, and is therefore only placed here on account of its spa-
thulate termination, which differs so much from that of the shell
with which it has been confounded, namely A. subradiatus.
Probably this is the A. subradiatus of D’Orbigny, T. J. pl. 118.
figs. 1 & 2.; but if so it differs so much from his A. subradiatus
previously referrred to that we feel justified in proposing a fresh
name for it. Our specimen is the only example we have met with
with the termination: still it is not an uncommon fossil near Sher-
borne, though it occurs very sparingly at Bradford Abbas and Half-
way House.
Fig. 4.—Termination of Ammonites Gervillii, Sow.
9. A. Gervitim, Sow. p. 184, tab. A. fig, 3; D’Orb. pl. 140..
figs. 1-7. (Fig. 4.)
This is a shell with a very curious and interesting termination,
which we have named delphinulate, because its side view 1s so much
like that of the head of the classic Dolphin. Sowerby says, ‘‘ This
64 J, BUCKMAN ON AMMONITES FROM THE
species occurs in a marly limestone which is replete with grains of
iron ochre. It is from Bayeux, in Normandy ” *.
Fig. 5.—Ternunation of Ammonites Brongniarti, Sow.
= yy
10. A: Bronentartr, Sow, t. 84 A, ‘ie. 2: DiOrcbampiaailane
figs. 1-5. (Hig. 5.)
The lip of this shell is so decidedly distinct from the preceding that
we cannot help separating them, although we at one time inclined
to a different opinion. It is not at all so complicated, but is of a
semilunar or, rather, semicircular shape, with a deep depression be-
neath, but without the elaborate form of the lip of A. Gervilla. It
is met with at Bradford Abbas and other places near Sherborne.
11. A. Mawserit, Buckman, n. sp.
Is perhaps related to the A.-Brocchi group ; but the fineness of its
ribs and the absence of tubercles is a sufficient distinction. We
have in one single example the usual deep depression before the
terminal semicircular depression. We possess several examples of
this shell from Bradford, Chaleombe, and other places ; but only the
one sent is an example of the termination.
12. A. Humenrimstanus, Sow. t. 500. fig. 1; D’Orb. pl. 133 & 134.
(Fig. 6.) | |
This is a very variable shell, sometimes having few (perhaps five)
thick whorls, at others from eight to ten, exceedingly slender and
delicate; yet the markings are the same, and the termination of both,
starting from a deeply contracted furrow, is simply semilunar in
shape, and is the same in both large and small examples.
This is a common shell about Sherborne, but is rarely met with
at Bradford or Halfway House.
* Sowerby, Min. Conch. vol. u. p. 190,
INFERIOR OOLITE OF DORSET AND SOMERSET. 65
Fig. 6.—TZermination of Ammonites Humphriesianus, Sow.
SS
a. Krom the side. 6. From the front.
13. A. Mooret, Lycett, ‘The Cotteswold Hills,’ pl. i. figs. 2, 7.
The flexure of the mouth of the shell, with its elegantly curved
line, like that of a modern Nautilus, is distinctive of this shell. It
is common to the sandy part of our Oolite below the usual Cepha-
lopoda-bed. The mouth is simply a termination of a flat slightly
ribbed shell, without any previous depression. It is a common
shell in the limestone bands below the Cephalopoda-bed ; but the
specimen sent is the only one in which we have observed the com-
pletion of the mouth of the shell.
Fig. 7.—Termination of Ammonites Moorei, Lycett.
e
We.
14. A. Boscrnsts(?), Reynés.
We quote this, with some degree of hesitation, from Beneke, inas-
Q.J.G.S. No. 145. F
66 AMMONITES FROM THE INFERIOR OOLITE.
much as we have only a single specimen. This, however, is from
the Cephalopoda-bed of Bradford Abbas, and in some points it is so
much like the A. Moorei, both in its form and the outline of the
mouth, that even now we must confess to fecling great difficulty in
the matter.
Note.—Since the above was in type, we have found other species
and examples with terminations. ‘These, with the new forms, will
described in a paper now preparing for the Society :
_ Discussion.
Mr. Cuartesworta called attention to the early work in this
direction of the late Mr. Chaning Pearse, who studied the Ammo-
nites of the Oxford Clay of Christian Malford. That author was
led to believe that the peculiar prolongations of the mouth were
periodically absorbed and reproduced.
ABNORMAL GEOLOGICAL DEPOSITS IN THE BRISTOL DISTRICT. 67
7. On AxsnormMat GrotocicaL Deposits tn the Bristot District.
By Crartes Moors, Esq., F.G.8. (Read November 17, 1880.)
In making excavations at Redland, on the edge of Durdham Down,
about 45 years ago, some conglomerates, associated with Carboni-
ferous Limestone, were opened up, which contained the teeth and
scattered and broken bones of reptilia, described by Messrs. Riley
and Stuchbury in the ‘ Proceedings of the Geological Society’ for
1836 under the names of Thecodontosaurus and Palcosaurus. As
they were then the oldest known reptilia and of a high order, much
interest has always attached tothem. <A few years since, in drainage-
works at the same spot, this conglomerate was again crossed, and
some other bones added to the series deposited in the Museum of the
Bristol Philosophical Society. The collection has since been reviewed
and described by Professor Huxley, F.R.S.*, and an account of
the physical characters of the district given by Mr. Etheridge,
LAI NES By g ;
Much uncertainty has prevailed as to the geological age of the
Durdham-Down conglomerate. At first it was supposed to be Per-
mian; but we have as yet no conclusive evidence of true Permian
beds in the West of England. Mr. Etheridge has placed it on the
horizon of the Dolomitic Conglomerate of the Keuper ; whilst, owing
- to the discovery by myself of the same genera of reptilia, under
somewhat similar physical conditions, in the Rhetic deposits of
Holwell, and since then of true Rhetic remains on Clifton Down, I
had referred them to the latter age—a point to be reviewed below.
In my paper on the abnormal conditions presented in the Frome
district I especially described numerous Secondary unconformable
deposits and vein-fissures resting upon or passing down through
the Carboniferous Limestone, some of them haying organic remains
whereby they could be referred to different geological periods.
Since then I have discovered several other features of interest at
Holwell; and as the phenomena of this district will serve as a
key to unlock hitherto unnoticed physical conditions in the geo-
logy of the Bristol area and some of the paleontology connected
therewith, it will be desirable first shortly to notice the special fea-
tures presented near Frome.
The Carboniferous Limestone has here its last south-eastern ex-
posure before being entirely covered up by Secondary deposits, and
is to be seen in very narrow ravines at the Vallis, Him, Mells, What-
ley, Nunney, and Holwell. The prettiest combe is that of the Vallis,
from which, at its northern end, bifurcates that which passes
to Elm and Mells. At the entrance to the Vallis at Hapsford the
first sections show irregularly bedded Rhetic conglomerates resting
* “On the Classification of the Dinosauria, with observations on the Dino-
sauria of the Trias,” Quart. Journ. Geol. Soc. vol. xxvi. (1870) p. 32.
tT “On the Geological Position and Geographical Distribution of the Rep-
tilian or Dolomitic Conglomerate of the Bristol Area,” Quart. Journ. Geol.
Soe. vol. xxvi. (1870) p. 174.
F2
68 CG. MOORE ON ABNORMAL GEOLOGICAL
in depressions on the edges of the inclined Carboniferous Limestone.
They are separated by thin blue clays with Avicula contorta and
also Discona Babiana. I have no doubt they would yield important
vertebrate remains, as I found a very perfect Dinosaurian vertebra ;
but, unfortunately, these beds have not been worked for some years.
Vertical mineralized infillings are present, passing down through the
Carboniferous Limestone in this section. In the southern corner, but
occupying a higher position than these conglomerates, there is a
patch of close-grained cream-coloured limestone undistinguishable
from the White Lias; but it has yielded me no trace of organic re-
mains. The deposits of one section usually differ from those in
another, or die out altogether, although they may be in close proxi-
mity. For instance, in the next quarry the conglomerate is a single
thick, dense bed, with pebbles united by calcareous matrix, in which
are occasional nests of Lstheria minuta and insects, whilst above are
a few inches representing the Lower Lias, capped by about 10 feet of
Inferior Oolite.
In addition to the unconformable Secondary deposits which lie on
the Carboniferous Limestone, a special feature of the latter formation
is the many vertical fissures passing down through it, with infillings
containing Secondary remains, or those of a still later age. In the
Vallis these veins are best seen in the face of a large quarry at Ege-
ford, where, in addition to several smaller ones, the workings are
bounded by veins at both ends, that on the north being of some
thickness, and showing a vertical side about 50 feet in height, where
it meets a patch of Inferior Oolite. The matrix of this vein is Liassic ;
and numerous organisms may be traced init. All the veins are much
mineralized, and contain sulphate of barytes in concretionary layers,
with occasional traces of galena and blende. At Elm and at Nunney
hematite iron-ore has been extracted ; at the latter place in close
proximity to a deposit of Inferior Oolite.
The hamlet of Holwell occupies a depression at the southern end
of the Vallis gorge, and is on every side surrounded by sections
which, if looked down upon from a little distance, without closer
inspection, would appear to most geologists to be entirely composed
of Carboniferous Limestone. The road from Frome to Shepton
Mallet passes through this spot, and crosses the little stream from
which the hamlet is named. On the eastern side are two quarries I
have already described*, viz. :—that of the Marston road, in which,
within a few yards, are present stratified Inferior Oolite, Liassie con-
glomerate (with many organisms), and a thin band of Rheetic clay, all
resting on Carboniferous Limestone, with a thick vein filled with calc-
spar in their midst ; and also a large quarry below, with a face pa-
rallel to the stream, in which are to be seen many vertical dykes,
some with Rhetic and others with Liassic organisms ~. They present
much mineralogical variety ; and the somewhat impure limestone
* « Abnormal Conditions” &c., Quart. Journ. Geol. Soc. vol. xxiii. (1867)
p. 483.
+ A section of this has been given in ‘‘ Abnormal Conditions” &c., Quart.
Journ. Geol. Soc., 1867, p. 484.
DEPOSITS IN THE BRISTOL DISTRICT. 69
within the veins shows, by its frequently being in very thin lamine,
that it has been deposited slowly. It is desirable to bear in mind,
whilst comparing the same facts in the Bristol district, that in the
quarries above noticed the limestone of these Secondary infillings is
often left standing out as butresses by the workmen, whilst they
work back between them for the purer Carboniferous beds.
Postpliocene, Liassic, and Rhetic Deposits. The Microlestes-
Quarry.—On the Shepton road, immediately west of the hamlet,
there is a large quarry on each side facing the road. The first,
on the south, is the Microlestes-quarry; in the other, inclined
Carboniferous Limestone has been worked between thick veins of
Middle Lias, the matrix of which occasionally showed carbonate of
lead and barytes. The rubbish-tippings from the limekiln have
since obliterated these points; but I have preserved them in pho-
tographs. It is probable that all the veins on this side of the
hamlet differ from and are to the south of those in the large
section east of the river.
In my former examinations of the Mcrolestes-quarry I was told
by the workmen that they had occasionally crossed a fissure down
which, by the aid of a rope, a man might descend; but, as it was
becoming dangerous, it was filled up. From this I have suspected
the presence of a Postpliocene cavern at the spot; but although it
has not been found, they have worked back upon a vein filled with
bones, which I have lttle doubt may be connected with one. It is
about a foot in thickness, and, like all the other fissures and their
infillings, appears to have its own special individuality. Like an
ordinary mineral vein, the walls have vertical mineralized layers, the
innermost being large crystals of dog’s-tooth spar. Towards the top
there are anguiar pieces of Carboniferous Limestone, which below
sive place to material composed of about one third of brown marl,
crystals of carbonate of lime, and dismembered jaws and bones of
Arvicola and frogs, with, rarely, small vertebree of birds and fish.
The jaws of Arvicola are very numerous, whilst their vertebree and
other bones are scarce. They appear to belong to A. arvalis or A.
saxatilis. Bones of the larger mammalia, though few, including ox
and deer, were found. Amongst them was found a tooth not to be
distinguished by itself from a human incisor; but the subsequent
discovery of the remains of wolf leads to the inference that it may
belong to that animal, the difference in the incisors being with diffi-
culty distinguished. Several Rhetic teeth, showing from their worn
condition that they are derived, and a few Carboniferous-Limestone
corals and shells are mixed with the above, as ; well as pebbles of
hematite and bog-iron ore.
The deposit, with its Rhetic remains, was in a north-and-south
fissure a little west of the above; but it is now all but exhausted.
_ Without reference to other mineralized veins in which no organisms
have been found, it will be seen that at Holwell alone, and in the
line of a single quarry of but a few hundred feet length, Post-
pliocene, Liassic, Rheetic, and Carboniferous-Limestone formations are
represented. ‘These later deposits are the rule, not only where they
C. MOORE ON ABNORMAL GEOLOGICAL
70
~>,
‘sdagg Axren%
LORS
*‘q1g0dep
uel ado
“OnAdTIOM
‘umog moypung fo abpy ay, yo worn
ay
—"T “OL
“£urend
DEPOSITS IN THE BRISTOL DISTRICT. Tt
fringe the outcrop of the clder rocks, but high up on their table-
lands, as in the case of the Charterhouse lead-mine, near
Cheddar.
Tue BristoLt AREA.
Before proceeding with a description of the Bristol area and
comparing it with the above, it is desirable I should advert to a new
palzontological feature which hitherto has not attracted any atten-
tion, in the presence of a multitude of minute Serpula-like calcareous
tubes found in various deposits under examination. Years ago I
noticed them in the freshwater brick-earth of Salisbury, which is of
Postpliocene age, and put them aside as minute Serpule; but after-
wards learning that all species of this family are marine, I thought
they might possibly be analogous to caddis-cases, and belong to some
insect. When they were afterwards found in enormous numbers,
and under many diverse circumstances, I saw the desirability of
learning more about them, and sent them to friends who were
authorities in special departments of natural history for their
opinions, at the same time describing the circumstances under which
they were found. Without mentioning names, it proved a “ pursuit
of knowledge under difficulties.” First, they were doubtfully re-
ferred to the cases of some Dipterous insect ; and if not such, it would
be worth considering if they were Serpule. An entomologist decided
that they were not insect-tubes; a good microscopist was of opinion
they were the calcareous cases left by rootlets of vegetation passing
down from the surface; next, an eminent zoologist intimated, with
some uncertainty, that they somewhat resembled the genus of Ser-
pulide, Filograna; then a good botanical friend and microscopist
pronounced them to be vegetable; upon which I sent them to a
first-class botanical expert, who was of opinion they had nothing
to do with vegetables, and that he had consulted a zoological friend,
who also believed they were worm-tubes allied to Annelids, and
that again they presented some resemblance to /ilograna.
They are to be found very abundantly in some of the vein-
fissures of the Carboniferous Limestone (to be referred to hereafter)
in the Bristol district, and also, though not in such numbers, in
some of the later stratified marls. My impression is that they
are due to freshwater conditions, and that, though they may not
be rootlets which have passed down from the surface (some of
them being found under conditions apparently precluding this idea),
yet they may, notwithstanding, be due to freshwater vegetation.
They are sometimes free, but often in clusters united by the ma-
trix of the deposit. It will be desirable to determine their syste-
matic position, as they will have a bearing on the age and other
conditions of the deposits in which they are found. I propose
that they should be recognized under the designation of Tubutella
ambigua.
Durdham and Clifton Downs.—I now propose to show that the
same physical conditions prevail at Durdham Down and at various
outlying spots near Bristol, as in the Frome district. The area to
72 C. MOORE ON ABNORMAL GEOLOGICAL
_be first noticed will be that embraced in the southern escarpment of
the Carboniferous Limestone, extending from Redland, its eastern
end at Durdham Down, to the suspension-bridge at Clifton, over-
looking the river Avon on the west.
Near the Old Black Boy inn, just under the edge of Durdham
Down, there are places known as The Quarry and The Quarry
Steps (see fig. 1). comming on the latter, we look down into a large
excavation, which musi have been formerly extensively worked for
stone, but is now occupied by small houses and gardens, most of which
are probably a century old. One of these houses is close under the
flight of steps leading to The Quarry, and has been built against a
natural vertical wall of mottled red or yellow unstratified limestone,
differing altogether in colour and texture from the grey Carboniferous
Limestone of the district, by which, on either side, itis bounded. It
is about 8 feet in thickness, and may be traced on the east side of
the excavation by its brighter colouring; and there is no doubt that
it continues into the limestone of Durdham Down immediately above.
As was the case with the workings on the Mendips, the old quarry-
- men here extracted the purer limestone, leaving the impurer some-
what conglomeratic infillings standing out, and terminated their
quarry on the east by this large dyke. As it has not been opened
up, little examination could be given to it for organic remains, which,
from its close proximity to the Thecodont deposit, would have been
desirable; but that some are present therein is sufficiently indicated
by the fact that, after examining a few pounds weight of the softer
material taken from the interstices or sides of the vein, I obtained
numerous minute fragments of bone or teeth, one very small fish-
tooth, an Hchinus-spine, a few joints of Carboniferous-limestone
Encrinites, and some of the tubes previously referred to.
The platform of the Quarry Steps rests upon the surface of the
above dyke. Looking from it, along the Down escarpment to the
west, the eye takes in Bellevue Terrace, on the edge of the Down ;
and it was between these houses and the quarry, a distance probably
of 200 yards, along the same face of limestone and on the same
horizon, that the deposit containing the Thecodontosaurian remains
was found. Unfortunately the precise spot is unknown; and, from
its being built over, there is not much hope of its being again
identified.
My late friend, Mr. W. Sanders, F.R.S., of Clifton, gave me, some
years ago, a sketch showing the conglomerate on the edge of the lime-
stone, with what was then considered to be New Red Sandstone at its
base (fig. 2); and it is significant that he does not so much represent
it as a basin-shaped depression in the limestone as indicate a deposit
following the slope of the escarpment, similar to the case of a vein
the top of which was opened up, but from which the limestone still
resting below against its side had not been removed. Mr. Sanders
also marks the spot where the reptilian bones were supposed to be
found. .
At the time when these reptilia were discovered, the peculiar
conditions of deposition I have indicated were unknown. In the
DEPOSITS IN THE BRISTOL DISTRICT. 73
Fig. 2.—Sketch Section of the Thecodontosaurus-bed of Durdham
Down. (Drawn by W. Sanders, Esq., F.R.S.)
Cis Pretest BORE SEAC
< ZING ‘ Z
NY iN ENG ZG
RS yy 4, Y, es OX
COw: aN Oe & G
“nN NEE N UAW <4 SO OX
Sf
ON,
a. Conglomerate of New Red Sandstone.
b. Locality of Thecodontosaurus. c. New Red Sandstone.
d. Carboniferous Limestone.
section described below, which embraces a line of working from the
Quarry Steps to a large quarry which I call the ‘‘ Avenue Quarry ”
(from its being immediately north of the Avenue Road), a distance
all together of about 680 yards, I shall show the presence, as at Hol-
well and elsewhere, of a series of veins with infillings derived from
different geological ages; and my interpretation of the reptilian
deposit therefore is that it 1s one of such a series in Carboniferous
Limestone, by which, on both sides, it is surrounded.
Durdham Down Section.—From the Quarry Steps to the end of
Bellevue Terrace, within which area the reptilia were found, is about
300 yards. Until lately these were the last houses fringing the Down
to the west; and there then stood up by itself, like a wall, a large
vein-infilling (the limestone having been worked up to it on both
sides) separating the garden of the last house from an adjoining
quarry. Other buildings have now occupied the line of the quarry,
covering up four smaller veins; but the one above referred to, from
14 to 16 feet in thickness, is still utilized as a boundary between the
gardens. It has the same general hthological character as that at
Quarry Steps, but has occasionally small pockets of iron-ore, and is
more mineralized. I purposed to examine these veins closely for
organisms, but have been prevented.
Passing along the roadway from this quarry, the next vein seen
was one containing hematite iron-ore, at its thickest about 16 feet.
It had been worked up to the roadway on the edge of the Down.
At my last visit this also was being filled up, and a house built
across it.
Alluvial Veins with Inassic and Rhetic Remains.—For about
200 yards from the iron-ore vein the limestone has been unworked.
Following the road to a spot near the ventilating-shaft of the
Avonmouth Railway, an archway facing the road leads into the
Avenue Quarry, which presents some interesting features. For
many years a lump of seemingly stratified yellow marl had been left
in the bottom of the quarry, the limestone having been worked
74 C. MOORE ON ABNORMAL GEOLOGICAL
around it. Its presence often puzzled me; but there is little doubt
that it is due to an alluvial infillmg into a small limestone cavern,
and is connected with one of three thin veins of alluvial material
which are present in this quarry. A cavern was many years ago
discovered on the Down, containing, amongst other things, the
remains of Hippopotamus, which are now in the Bristol] Museum.
These three veins are filled with an ochreous or brown clay, which,
when critically examined in its natural condition, appears to differ
slightly in character in each, as though they might have received
their infilling at somewhat different times ; still, to save labour in the
examination of their contents, they were mixed together. Their
organic remains are very varied, and not less so their mineral con-
stituents. Their Postpliocene or still later age is indicated by the
presence in them of frequent portions of the incisor teeth of Arvicola,
and a single shell of Hew. Although all the remains are rare, those
from the Lower Lias are most abundant. These consist of young
forms of Ammonites of two species, Myacites and Astarte, Cylindrites
and portions of three other univalves, a Pentacrinite-stem, and a
single valve of an Entomostracon. ‘There are teeth and scales of
fishes, and a fragment of bone which may be either Liassic or Rheetic.
The interesting presence of Rhetic remains, however, is shown by
teeth of Saurichthys and Lophodus and a small palate identical with
species from Holwell. Some of the teeth are bleached and worn by
water-erosion. The little calcareous tubes accompany them.
The residue of these veins, after washing, shows a great abund-
ance of black pisolitic granules. The following analysis of its
mineral contents has been obligingly made by Mr. Gatehouse, City
Analyst of Bath :—
Soluble in acids:
Watery Mos) ioc ts Sisieoe Gade a Bee a 7°80
Calciumycarbonmate tame ar ae eee 20°50
Magnesium carbonate...... ee eB os 0°73
Oxide ‘Of Tromso.) eee os sil eens 6:50
Zime carbonate (calamine) 2-5. 02) 24.45 0°54
Manganese, dioxaideds saucy. a)-Nelcie cna 0-50
ead=sulphide\(eallena)) ye. eee 0°90
ho) Det Mra AUR eM NAME ie Bestia i ny'ss 6 8°16
PeMADNACUNGl: PREM ML HARE OIRO 6 oa.3 2°60
Pobassivamn'y 6,552.05 eng sieeucie ds oe ieee ne 0:07
. 48°30
Insoluble in acids:
Calcium sulphate............ Pale ee 0-39
SUHICALC Of, ZINC Cerrar. cele n anand eae 0-25
Oxadeyor ron Gnsoluble) ie; ariel 6°55
Alumina Pe ROMA NHRC MRO Wind suis ics 10°45
Silica RS UIM Rn NENTS Mae fee ka hes 33°70
WOPDCE MN ce cas walneal ele emete trace:
DEPOSITS IN THE BRISTOL DISTRICT, 75
Inassic Vein.—The working of the limestone in this quarry has ter-
minated on the western side against a vein from 10 to 12 feet thick,
which has received an infilling of yellow clay of an entirely different
lithological character from those last mentioned. So far as the evi-
“dence goes, it is apparently a vein of true Lower Lias, with occa-
sional weathered blocks of Carboniferous Limestone. All the remains
found are Liassic, and consist of :—
Teeth and scales of fishes. Gryphea.
Ammonites (young). Terebratula.
Univalves (several species). Cidaris (teeth, plates, and spines).
Astarte. Pentacrinites.
Modiola. Cristellaria.
Lima. Webbina.
Cardium
All the phenomena I have mentioned, from the Quarry Steps to
the Avenue Quarry, are embraced in less than half a mile. Without
including the Reptilian deposit, eleven veins are shown to be pre-
‘sent; and but for a considerable part of the edge of the Down being
covered, no doubt many others would have been seen.
The thetic Bone-bed—There are no workings between the
Avenue Quarry and the neighbourhood of the Clifton suspension-
bridge. ‘The road to the latter is cut through Carboniferous Lime-
stone containing many veins, which are usually filled with cale-spar
and other mineralized matter. Looking towards the Observatory,
there are two veins. One, filled with limestone, has been left boldly
standing up by the quarrymen; but nothing can be said of its age.
Close to the toll-house, however, on the Clifton side, there is a
deposit of considerable interest, having a face of about forty feet, in
which the Rhetic bone-bed and its associated remains are present.
It is partly composed of irony and yellow sandy-looking marl,
with many free crystals of carbonate of lime, as in the Holwell
fossiliferous infilling ; and there are also patches of finely laminated
rock, similar to the Rhetic “ White Lias.” Some of the associated
blocks of stone appear to be fossiliferous ; but as the deposit forms the
boundary-wall of the toll-house, they cannot well be broken down
for examination. The bone-bed is two inches thick, with teeth of
Saurichthys apicalis, Lophodus minimus, and many fish-scales; and
the clay on either side contains fish-remains of the same age.
In Professor Ramsay’s ‘ Physical Geology and Geography of
Great Britain, he has given a very pretty sketch of the Gorge of the
Avon, with the Suspension-bridge and its beautiful scenery, which,
through the kindness of Prof. Ramsay and of Mr. Stanford, the pub-
lisher, I am permitted to use (fig. 3). Curiously enough, it includes
the Rheetic bone-bed, and, on the shoulder of limestone looking down
the river on the east, the conglomerate mentioned below. The Car-
boniferous Limestone dips rapidly to the south under the Bedminster
coal-beds, and disappears under beds of New Red Sandstone. A
lighter line in the sketch, between the eastern abutment of the bridge
and the houses on the level of the roadway, with the Observatory
seen beyond it in the distance, shows the exact position of the Rheetic
deposit.
76 C. MOORE ON ABNORMAL GEOLOGICAL
Fig. 3.—Gorge of the Avon at Clifton.
Before referring to other outlying sections near Bristol, it may
be noticed that although the true New Red Marls are present
around, the red and variegated marls which lie on the east of the
basin between the Durdham-Down and Clifton escarpment, and
extend towards Bristol, are alluvial. They have been opened up in
brick-pits repeatedly, as well as the conglomerates below. From
the former, after long search, I obtained several small bits of Inferior
Oolite and fragments of shells of Ostrea. The conglomerates are
bedded, and are usually extracted on the site of each building
erected; and although hundreds of thousands of tons have been so
used, I have never detected any contemporaneous organism in
them, nor have I heard of such having been found. They get coarser
and more irony as they approach the limestone below; and in
several sections its rugged surface has received pockets of hematite
iron-ore. The pebbles are comparatively small and angular, and
give the idea that they may be due to a subaerial denudation of the
Carboniferous tableland above.
Conglomerate of the Avon Gorge.—Passing down the river, not far
below the Suspension-bridge, the ‘ Dolomitic Conglomerate,” of
which Mr. Etheridge has given a section, is reached. It rests on
the edge of the Carboniferous Limestone at the side of the road
leading up to the Down, and is, as a friend has remarked, ‘a
gigantic heap of conglomerate” with pebbles of great size at the
base, getting gradually smaller at the top. It is very irony, and
appears to occupy but a small area. Some red marls gathered from
DEPOSITS IN THE BRISTOL DISTRICT. 77
the sides and interstices of the deposit yielded me part of a fish-
palate, which is probably of Carboniferous-limestone age, and great
numbers of Encrinital stems, a comparatively recent freshwater
operculum, and numerous examples of Tubutella. Whatever may be
the age of this deposit, groups of the latter are usually surrounded
by an irony matrix which seems part thereof.
Vein at Ashton.—On the west side of the Avon, about a mile
beyond Ashton, considerable deposits of iron-ore occur ; but I have
been unable to examine them. They lie at the foot of the lime-
stone escarpment. On the tableland above them, at Longwood
Farm there are disturbed Carboniferous Limestones, in which a
vein occurs containing occasional lumps of galena and some ¢a-
lamine. Tubutella is present in great abundance. The upper
part of this vein is somewhat honeycombed; and the tubes are
found adhering to thin flakes of calc-spar. No other organisms
were found at this spot.
Westbury-on-Trym— Carboniferous Limestone with Minerals and
Oolitic Remains.—On passing from the Durdham-Down quarries
(previously mentioned) along the eastern edge of the Carboniferous
Limestone, at a distance of two miles, some large quarries are to be
found. On the eastern side of one at Southmead, worked by Mr.
Kennedy, there may be seen what appears to be an ordinary mineral
vein, about a foot thick, passing down through the section. It con-
tains good hematite iron-ore, ochre, galena, and calamine. Although
it appeared nothing but a mass of mineral matter, I still hoped a
sample might yield some evidence of its age. In this I succeeded
beyond my expectation; for on washing it I at once found many
angular pieces of Inferior Oolite, which, from their being stained
with iron, were not before visible. On a still closer examination
I obtained the oolitic organisms given in the list below, asso-
ciated with TZwubutella; the specimens show very little sign of
attrition. No Oolitic deposit from which they could be derived,
however, is in this district nearer than Dundry, six miles to the
south, or the Cotteswolds, many miles to the east, with, in the latter
case, the area of the Bristol coal-field intervening.
In the same quarry there is at another spot a pocket of light-
green clay. Although very intractable, I was able to disintegrate
it sufficiently to find that it contained Alge &c.; and although
there remains a little doubt as to their age, it is hkely they are of
comparatively recent date.
Westbury vem, Oolitic Organisms.
Fish-tooth. Thecidium.
Nerina. Bryozoa, several species.
Solarium. Echini, teeth, plates, and spines.
Univalve, sp. Entomostraca.
Turbo. Serpule.
Dentalium. Foraminifera ?
Astarte, Tubutella,
Cardium. Pentacrinite joints.
Ostrea. Encrinite stems, Carboniferous.
Algeze (in clay vein), several genera
78 C. MOORE ON ABNORMAL GEOLOGICAL
The sections remaining to be noticed are along the eastern edge
and to the north of the Bristol coal-field. On the eastern side the
Carboniferous Limestone does not come to the surface between the
Mendips and a very small outcrop at Grammar Rock, under Lans-
downe, near Bath (which is not recorded on the Ordnance Map), and
others at Wick Rocks and Codrington. From Chipping-Sodbury
a narrow belt continues to Yate snd Wickwar, and entirely sur-
rounds the north of the coal-basin.
At Wick, where the quarries are extensively worked, mineral
veins are to be seen having their usual vertical bands of barytes,
galena, &c. passing down them. In their softer pockets Tubutella
is abundant; in one which has a marly infilling it is present in
great numbers. Occasionally small patches or pockets of grey marl
lie near the surface; but I have not yet found any other organisms
in them.
The Yate Rock Sections—These are between Chipping Sodbury
and Wickwar. On the ragged surfaces of the limestone there are
here also pockets containing more mineralogical materials with
Tubutella. A vein passes down from the surface of one of the
quarries a foot in thickness, containing soft mineralized material in
which are myriads of these little tubes; they are often attached to
the broken-up pieces of barytes and other minerals.
Netilebury Quarry, Yate, and Clevedon.—The Nettlebury quarry
is a large one, nearest Wickwar, and is the last I shall refer to on
this side the Bristol coal-basin. A section of it has been given by
Mr. Etheridge *, in which are shown to the east horizontal step-like
beds, overlying highly inclined Carboniferous Limestone, whilst
on the west side equivalent beds dip at the same angle as the
limestone towards the coal-basin. At the present time it would be
difficult to recognize the locality from the above section, from the
almost entire absence of the beds on the eastern side, though
they are present from 12 to 14 feet thick on the west. Mr.
Etheridge considers these beds to be of the age of the Dolomitic
Conglomerates, and the representatives in lithological condition and
age of the supposed Magnesian Limestones of Clevedon. The latter
are thick, irregularly bedded, yellow limestones, used in the district
for building-purposes. It is apparently a local deposit, resting in
the quarry near the hotel on Old Red Sandstone, which crops out on
the beach and abuts against Carboniferous Limestone to the east, the
Old Red being fringed on a level with the Severn by a continuous
belt of Dolomitic Conglomerate, continuing north for some miles. .
Almost every parting or crack between the blocks of Clevedon
stone shows the presence of galena, carbonate of copper, or other
minerals. In only one instance have I found a block of stone with
organic remains. This contained afew Encrinital stems, an im-
perfect Rhynchonella, and also several imperfect Strophomene. Were
it not that the specimens put on the lithological appearance of the
enclosing matrix, I should be disposed to think them redeposited
* Quart. Journ. Geol. Soe. vol. xxvi. (1870), p. 179.
DEPOSITS IN THE BRISTOL DISTRICT, 79
from the Carboniferous Limestone *.” Looking at the Yate deposit as
it lies on the limestone in the section, it has much resemblance to the
Clevedon beds, but on closer examination this ceases. The latter
are almost pure Magnesian Limestone, whilst the upper 9 feet of
the former are of sandy yellow marls, which on being washed float
away and leave a sandy residue. Next follow eighteen inches of
yellow limestone, in two irregular beds, which in structure and
colour somewhat resemble the Clevedon stone. On treatment with
acid these also leave a sandy residue. Between the above and the
Carboniferous beds there is a thin deposit in pockets, almost com-
posed of fine grey sandstone. There are no organic remains special
to these beds beyond fucoids and Tubutella ambiqua, which is rare.
For these reasons, and knowing how varied are the deposits on the
outcrops of the older limestones, I am disposed to think that the
yellow beds at Yate are of comparatively recent age. On the
surface of the Carboniferous Limestone there are occasional thin
patches of what appears to be a comminuted shelly breccia with a
grey sandy matrix, which I do not think the equivalent of the
bouldered Dolomitic Conglomerates found in other parts of the
district.
Thornbury Railway and Secondary Veins—The branch line which
leads from the Yate station to Thornbury exhibits some interesting
geology. At Tytherington fine sections of Carboniferous Limestone
are seen, and thick deposits follow of what are, no doubt, true
Dolomitic Conglomerates. On emerging from the tunnel towards
Thornbury these have some marly divisions, in which, in a flat over
the tunnel, some galena has been found. Not far beyond, the Lower
Limestone shales pass into the Upper Devonian beds, the conglo-
merates also resting upon them. Just before reaching this point
there are several thin veins in the limestone containing sulphate of
barytes and galena, in a matrix of gossany iron-ore. A sample
from the soft ochreous part yielded me three Conodonts of Carboni-
ferous-limestone age—and of Secondary remains, Pentacrinite joints
and a single specimen of a Foraminiferous shell, Planularia pau-
perata. On a second visit I discovered deposits towards the surface
which, lithologically, I cannot distinguish from a ferruginous marl
of the Middle Lias, which contains hollow casts of shells and crushed
specimens of what appear to be Rhynchonella tetrahedra. Tubuiella
is present in great numbers, surrounded, as at Yate Rocks, by a re-
deposited ferruginous matrix.
Age of the Deposits—From the foregoing examples of abnormal
deposition, all of which have been accidentally revealed by quarrying-
* Since writing the above, I have sent the specimens to my friend Mr.
Davidson, who says:—‘‘ The specimen you send for my examination you say is
from the Magnesian limestone. In colour it looks like a rock of that for-
mation ; but I have never hitherto seen from our British Permian rocks a Sfro-
phomena or Streptorhynchus shell similar to the one I observe on both sides of the
specimen, and which looks like Strophomena crenistria. 'The Rhynchonella is
not sufficiently complete for specific determination. If not Carboniferous, at
least one of the species would be new to our Permian rocks or Magnesian Lime-
stone. I almost fear your enclosed specimen is Carboniferous.”
80 C. MOORE ON ABNORMAL GEOLOGICAL
operations in the Carboniferous Limestone, it must be manifest that
there are a multitude of other examples not yet opened up that
would yield an interesting study to the geologist. One of the most
difficult problems regarding some of them is to arrive at satisfactory
conclusions as to their exact age; but there can be little doubt
that the physical conditions to which the deposits are due were the
same both in the Bristol and the Mendip areas. Supposing the
fissures in any district had all been caused by the same shrinking or
change of level, they would have been subject to the same refilling
influences, and would contemporaneously have received a mixture
of materials derived from the denudation of that time; but although
the alluvial infillmgs in the Avenue Quarry have a mixture of
organisms, it is a singular fact that in a series of parallel veins
coming to the surface on the same horizon, not far removed from
one another, and some of them but a few inches in thickness, each
appears to have an individuality of its own, and to represent in
geological time intervals clearly distinct from one another. As at
Holwell, so at Durdham Down, the worked face of the escarpments
reveals infillings of allnvium, Oolite, Lias, and Rheetic and Keuper
beds, whilst mineralized or iron-ore veins show conditions specially
their own.
Reference has repeatedly been made to the Tubutella ambiqua,
which I have found in almost every deposit that could be examined
under favourable conditions, from Maidenhead to those of Gloucester-
shire and Somersetshire. When they occur, as in the brick-earths
of Salisbury, in association with freshwater shells, and also with
Postpliocene mammalia, there seems little reason to doubt that
they belong to freshwater deposits. If they can be traced in older
formations, they may be a guide in determining the conditions under
which those formations have been laid down. I have reason to
suppose this may be the case between the Upper Devonian and the
Carboniferous series. All veins, mineral or otherwise, come to the
surface; and if the Tubutelle be found therein, they will probably
indicate the presence of freshwater conditions. ‘The upper portions
of those I have mentioned in this district represent the gossans of
the lodes in more ancient rocks ; and if, as at Yate and Tytherington,
the Tubutella is caught up or surrounded by the mineral matter of
the vein, there has either been a remodification of that portion of
the vein, or it must have been contemporaneous with the organisms
enclosed. 7
I have already shown that most of the mineral veins of the
Mendips and South Wales are at least of Liassic age; and on this
point I have much confidence in the belief that a careful exami-
nation of the gossans and other mineral constituents of the veins in
our more ancient rocks will repay the labour, by giving either more
precise indications of their age or of the physical conditions under
which they were deposited.
Age of the Bristol Reptilia.—The varied points mentioned in this
paper have drawn me away from the chief object which led to their
consideration, viz. the age of the Bristol reptilia. As before
DEPOSITS IN THE BRISTOL DISTRICT, ont
remarked, the peculiar circumstances attending their discovery has
always left this in some obscurity. They are now assigned by
Mr. Etheridge to the Dolomitic Conglomerates at the base of
the Keuper. ‘These conglomerates are in great part composed of
rounded boulders of the Carboniferous Limestone, some of them of
great size, and seemingly requiring glacial conditions for their
removal and transportation. Not only do they fringe the outcrops
of the limestone from which they are derived, but they form an
almost continuous deposit of considerable thickness, extending for
many square miles in the Somersetshire coal-basin, the inclined
ragged limestone edges of which are, in places, rendered by their
denudation quite horizontal. The removal and redeposition of the
conglomerates indicate very troublous times, during which it seems
impossible for any organic life to have existed; for nothing could
have withstood the grinding-processes to which it would have been
subjected ; and it is a significant fact that no organic remains have
ever been referred to this period except the reptilians under notice.
For these reasons, and from my having found the teeth of The-
codontosawrus and Palcosaurus in the Rheetic deposit at Holwell,
and also from my subsequent discovery of the Rhetic bone-bed and
remains of that age almost alongside the Clifton reptilia, I had
come to the conclusion that the latter belonged to this period—a
view which further investigation respecting both Keuper and Rheetic
reptilia requires me to modify. Seventeen Thecodont teeth, more or
less perfect, are in my Holwell series. On comparison with those
from Bristol, they are more robust, have a more wrinkled or
striated surface, with the serrations on the edges smaller, less
oblique. and more numerous. In my paper ‘‘On Abnormal Con-
ditions” &c.*, I gave a section of variegated Keuper marls at
Ruishton, near Taunton, one bed of which I described as a “ Gritty
conglomerate, with occasional sandy bands and intermediate layers
of marl, with fish, reptile, and batrachian remains, fourteen inches
thick.” In this bed I have lately found some teeth of T'hecodonto-
saurus, which appear in all respects identical, in form, structure,
and the character of the serrations on their edges, with those from
Bristol. It contains also Acrodus keuperinus, Hybodus, Diplodus,
&e. Itisrather a coarse sandy bed than a conglomerate; and, owing
to its being rather unconsolidated, its remains are very fragile.
There seems little doubt that this bed is on the horizon of that in
Warwickshire which has yielded identical vertebrata; and if so, the
Bristol reptilia will have to be removed one stage later in time, from
the Dolomitic Conglomerate to the middle of the Upper Keuper.
Té is an interesting paleontological fact that, although most of
the generic forms of the Keuper recur in the Rheetic beds, so far as
I have ascertained, the species differ, and are special to the two
formations.
* Quart. Journ. Geol. Soc. vol. xxiii. (1867), p. 468.
Orie G.c. No, 145. G
82 ABNORMAL GEOLOGICAL DEPOSITS IN THE BRISTOL DISTRICT.
Discusston.
The PresipEent spoke of the great industry and skill of the author
in collecting the evidence on which this paper was based.
Mr. Tawney stated that Mr. Sanders held that the Dolomitic
Conglomerate is of different ages in different parts of the district,
and that the Vhecodontosawrus is high up in the Keuper series. He
thought that the fact of these remains being imbedded in solid con-
glomerate was scarcely reconcilable with the notion that they came
from vein-infilling.
Dr. Duncan, with reference to the origin of the so-called Tubu-
tella, stated that similar tubes might be seen in course of formation
by the escape of air-bubbles from the surface of oysters and other
shells covered with Algze in turbid water containing carbonate of
lime.
Prof. Sretny spoke of the great interest attaching to the question
of the age of the Thecodontosawrus. He considered the specimens
exhibited to belong to at least two genera. He stated that the ilium
of Thecodontosaurus is Crocodilian, with Dinosaurian affinities.
Rev. H. H. Winwoop supported the views of the author concerning
the position of the veins of Durdham Down. He remarked upon the
difficulty of understanding the mingling of different faunas in the
same vein.
The Presipent supported the views of Mr. W. Sanders, as ex-
pounded by Mr. Tawney, and bore testimony to the great value of
Mr. Sanders’s map of the Bristol area.
The AutHor agreed that the Magnesian Conglomerate is of diffe-
rent ages. He thought the Thecodontosaurian remains were ob-
tained from the top of one of the veins. He stated that, while the
veins occasionally contained the remains of fossils belonging to more
than one geological period, others contained organisms which
appeared special to a single period only, implying a denudation and
refilling in veins, at the present time difficult to account for.
J. W. CARRALL ON CHINESE CARBONIFEROUS PLANTS. 83
8. Norzs on the Locaritry of some Fossits found in the CARBONIFEROUS
Rocks at T’ane Suan, Cuina. By Jamus W. Carratt, Esq.,
F.G.S. &c., of H. 1. M. Customs Service, China. (Read Novem-
ber 3, 1850.)
Tue fossils which form the subject of this paper were found at
T’ang Shan, Chiao Chia T’un, in Lan Chow of the Province of
Chih Li, and about 120 miles from the treaty port of Tientsin,
in a N.N.E. direction from that port.
A Chinese company has been formed, known as the “ Chinese
Engineering and Mining Company,” to work the bituminous coal
deposits there found on the European system.
Mining operations were commenced in 1878 by ascertaining the
locality of the coal-seams by boring with the diamond boring-
machine. The bore-holes, three in number, averaged about 40U feet
apart; the third and deepest of the three driven reached a depth of
536 feet.
The seams dip at an angle of 45° to the north, calculated by the
angle of the strata found in the bores.
The thickness of the coal-seams, not taken at the slant but
parallel to the beds, is as follows :—
ft. in
iNowi-seam, N. of King’ seam: o..4.... 6 O odd.
TSO? GOUT USS nO Ire el cee era Ibs
Wosileseam, o: of King seam ...... 5... Oued
No. 2 seam cy Mn a ete ec ie Ra Ia nd
No. 3 sear ey abla Meeps ONS ae oe Oe Id
No. 4 seam Boy) 1 aI ae ae ere ALD
The seams are in curves or folds; one seam that comes to the
surface at the back of the colliery, again appears above ground
halfway from the colliery to Kai Ping (say three miles from the
first outcrop), and again five miles further on, trending in a north-
erly direction.
Some very good magnetite, containing between 45 and 8U per cent.
of metallic iron, has been found at Pai Mah Shan, about seventeen
miles from T’ang Shan. It is intended to erect roiling-mills near
the colliery, and place them also under foreign superintendence,
trams being laid down (after permission has been obtained) between
Pai Mah Shan and the hills for the transit of the ore.
The most striking feature of the geological formation of the
country round ‘l’ang Shan is, that above the Carboniferous system
is first loose sand and then loam, the loam being uppermost, and
extending but deepening all the way to Tientsin. Decomposed
red sandstone was seen in the distance to the north.
A gradual ascent commences four miles before coming to Lu
T’ai by land from Han Ku, and continues all the way to T’ang
Shan. The colliery is situated in this incline, and is about a mile
84 J. W. CARRALL ON CHINESE CARBONIFEROUS PLANTS.
from the nearest hill, T’ang Shan, which I do not think is higher
than 300 feet or thereabouts.
From the roundness of the hills and the way the chain is detached
in places, there is not the least doubt in my mind that this part of
the country was under water, and 1s now gradually rising, this also
being proved by the fact that, according to Chinese history, the city
of Tientsin was at one time situated on the seaside, and itis now some
twenty-five miles inland.
Note on the Specimens, by W. Carrurumrs, Esq., F.R.S., F.G.S.
The specimens from China belong to a single species of Annularia ;
and I have no doubt that it is A. longifolia, Brongn., which is so
abundant in our coal-measures in Britain, and is found on the con-
tinent and in North America. It occurs throughout the whole of
the coal-bearing beds, from the lowest to the highest.
Newberry and others have described fossil plants from China asso-
ciated with beds of coal; but these belong to Trias or still later
formations. The great interest of this communication is that it
records the existence of the true coal-measures in China, and gives
a range to a well-known Carboniferous plant, in harmony with what
we already know of other western contemporaneous Paleozoic
plants.
DISCUSSION.
THe PrEstipent remarked on the great interest attaching to the
discovery of these Coal-measure fossils.
Mr. Carrurners pointed out the interest attaching to the com-
mencement of coal-mining in China. He remarked upon the world-
wide distribution of certain Paleozoic species of plants.
Pror. Jupp spoke of the importance of this discovery in a country
the geology of which was so little known.
Mr. Branrorp suggested that possibly future observation might
show that these plants were associated with Mesozoic forms.
The Palseozoic flora had not a worldwide distribution. Mesozoic
types of plants had been observed in Australia in Paleeozoic beds.
Pror. Seetey demurred to the conclusions of Mr. Carruthers as
to the distribution of Paleozoic plants.
Mr. Buaxs supported Mr. Carruthers’s views.
Mr. Carrutuers, in reply to Mr. Blanford, said he believed that
the Glossopteris-beds of Australia are really Mesozoic and not Palee-
ozoic in age. .
Mr. Buanrorp said the late Rev. W. B. Clarke had found Glos-
sopteris-beds intercalated amongst Paleozoic marine fossiliferous
beds in coal-pits in New South Wales.
THe PRESIDENT supported the views of Mr. Carruthers and Mr.
Blake, in opposition to those of Prof. Seeley.
Pror. Jupp supported Prof. Seeley’s views as to the existence of
life-provinces in Palzeozoic times.
tor Ho
fl
Geol. Soc. Vol. XXXVII. PLV.
WIGS
_ 400 te.
yf /
Bagshot “Sands
‘s tation.
How-ledge
Lime: stone
RL Lyne
Ue Dangertield
|
:
1 Lith 20 DPB d. S* Coven S* Covent Garden
786
:
e
¥
bat
é .
\\
‘ i
peels
,
‘ i
;
2
2
\
<i
z ee ee = ee ee es : La = — tntcart. Journ. Geol. Soe. Vol. XXXVIL FL
|
/
SECTION OF THE GILINEIRS IN TROMME/AIN(D) ANID) = OIL TE TEIL, ANS), = WISI =) WHIT
' W/6? E<— > Wiss.
H Headon Hill
OT ft.
if 0 t 1 a nr d B a y = . 2
i Gravel
|
i
| 200 # ee
' Thick Lymna@a
Teclend Bey Firting Ree
| = : Bote a
Z Vera bed: ;
GCrio-bed gs C12 i How Ledge limestone Neritina -bed
Varden sands Wardein sands
G 0 Zz n e l L I @ v
:
} = N 10° E<—> S95 W VIGE SBY
were ji 4 NIGE<—> S16°W
i Warden. Battery (Eoerbeppenth
: pe Bramble Post- Tertiary Gravel cap eer
Petiory Linstone Colwell Limestone
—— ee U. Head: Np eee U. Heador Chine = : ____ Me Headon
ee f Ue Sands & hazelnut bed » Hea ae z tipper ee ae —
} Grass slopes -
EN
= Sp 7 A > How Ledge Warder Chawa.-limestones
pero = TO ry : with Lymnea
Limestone = Cventricosaor bed. gime re = 5
0 prcpratan zone i Oyster Ledg:
bank
> ot 7 ani
Scale for Vertical Heights 2500. Scale for Horizontal Distances 5280, or 12 inches w the Mile (one inch 0 46 yards.)
aa ~ |
Fral® Dangerfield Zit: 22 Bedtord. S* Covent Garden
=e
get geile had
THE BEDS AT HEADON HILL AND COLWELL BAY, ISLE OF WIGHT. 895
9. On the Beds at Heapon Hitt and Cotwett Bay in the Isle of
Wight. By H. Kunrrne, Esq., and E. B. Tawney, Esq., M.A.,
F.G.S., of the Woodwardian Museum, Cambridge. (Read De-
cember i, 1880.)
[Puate V.]
I. InrRopuctIon.
In a recent communication laid before the Society* the opinion was
expressed that a serious error had been made by almost all previous
writers in regarding the marine beds at Colwell Bay and Headon
Hill as on the same geological horizon ; we read :—‘* We shall now
demonstrate that the Colwell-Bay marine beds are not, as has been
hitherto supposed, the equivalent of those of Headon Hill and Hord-
well Cliff, but that they occupy a distinct and much higher horizon.”
Upon the correction of this supposed error a new classification and
nomenclature for the Upper Eocene formation of Britain was pro-
posed. .
The author further, after a review of the paleontclogical evidence,
arrived at the conclusion that, on the one hand, the fossils in the
Headon Hill and Hordwell Cliffs were identical, while, in the second
place, those of Colwell Bay, White Cliff, and Brockenhurst presented
the closest agreement among themselves. Then, comparing the
former two localities, taken together, with the latter three, taken
together, he considered (1) that the fauna of the first group was
largely estuarine, and that of the second group marine; (2) that
less than half the forms found in the former occur in the latter; (8)
that the fauna of the former approximated more to that of the Barton
beds, having about one third in common with them, while not more
than one fifth of those from the latter three localities occur at Barton ;
(4) that the fauna of the former two agreed with that of a series of
beds on the Continent which underlay and were older than beds
containing the fauna of the last three.
In the following communication the authors attempt to traverse
these points in the paper above referred to, in succession. By reference
to detail-sections they argue that the stratigraphical evidence is
plainly demonstrative of the identity of the Colwell-Bay and Headon-
Hill marine series, the beds being continuous through the cliffs and
easily traceable.
Referring to the paleeontological evidence, it is shown from collec-
tions, made with their own hands this year, (1) that the fauna of the
Colwell-Bay and Headon-Hill beds are identical; (2) that this fauna
differs considerably from that of the Brockenhurst bed, which occupies
a lower horizon; (3) that the Colwell-Bay bed has less than one
third of its species common to Barton beds, while the Brockenhurst
fauna has nearly one half in common with Barton beds.
* «On the Oligocene Strata of the Hampshire Basin,” by Prof. J. W. Judd,
E.R.S., Sec. G.S., Quart. Journ. Geol. Soe. vol. xxxvi. p. 1387.
Q.J.G. 8. No. 146. H
86 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
We conclude therefore that no reason has been shown for upsetting
the classification of the strata adopted by the Geological Survey, and
which, for nearly a quarter of a century, has been received among
geologists.
Certainly we wish to uphold in its integrity the work of the late
E. Forbes *, and the classification of beds adopted by him when
Palxontologist to the Geological Survey, and subsequently confirmed
by Mx. H. W. Bristow, F.R.S., in the second Survey Memoir? on the
Isle of Wight.
One of the authors, from his long residence in the district and his
constant occupation with these beds, has been long satisfied that
E. Forbes’s account of the beds is true to nature, and his classification
fully borne out by lithological identity of beds, as well as by distri-
bution of the fossils. The present notes, then, are based on his part
upon an aquaintance with the district, and the work of the Geological
Survey there during its progress, supplemented by subsequent visits,
and specially this summer by a joint examination by both, including
measurement of beds and collection of fossils, which, however in-
complete, was made bed by bed, and represents the prevailing fauna
of each—a point on which we lay great stress.
We do not wish to delay over the history of previous opinion,
which has been sufficiently treated in Forbes’s and Prof. Judd’s
memoirs ; but the latest criticism of Forbes’s work (op. cit. p. 141)
may be alluded to.
II. Tornanp anp Cotwett Bays.
The Survey Horizontal Section east of Headon Hill_—The first
point at issue between Forbes supported by “ nearly all observers, ”
on the one hand, and Prof. Judd on the other, is whether certain
marine beds known as the Middle Headon (including the “* Venus-bed”
of local collectors) in Colwell Bay are rightly associated with similar
marine beds in Headon Hill. The Survey identify them, and
correlate the freshwater beds immediately above and below as Upper
and Lower Headon respectively in both localities. This succession,
however, is stigmatized (op. ct. p. 142) as a “ mistake ” of which the
‘‘ primary cause ” is considered to be an “ assumed” existence ‘“ of
a great anticlinal fold of which the summit is supposed to be seen
in Totland Bay. The manner in which this supposed anticlinal is
regarded as having affected the strata is illustrated in Prof. E. Forbes’s
memoir, pl. vii. fig. 1, and also in Sheet 47 of the Horizontal Sections
published by the Geological Survey. And yet further on we read
(op. ert. p. 146), “ at Totland Bay there is undoubted evidence of the
presence of a slight anticlinal fold having its summit near Widdick
Chine, to the westward of which the beds for a short distance have
a slight dip to the south;” so that after all the only mistake the
Survey could have made would have been to exaggerate the dip.
We are next told of the E. and W. flexure, which causes a slight
* On the Tertiary Fluvio-marine Formation of the Isle of Wight, by Prof.
E. Forbes, F.R.S., 1856 [Memoirs of the Geological Survey of Great Britain].
+ The Geology of the Isle of Wight, by H. W. Bristow [Sheet 10], 1862.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 87
dip to the W. in Headon Hill; and it is implied that the Survey
section is false, owing to the neglect of this consideration. We
must point out, however, that this Section, Sheet 47, fig. 2,in which
alone the anticlinal is shown, does not go through the summit of
Headon Hill at all, and passes about a half mile inland at the latitude
of Widdick Chine : init the Upper Bagshot beds are made to appear a
little above the sea-level at that spot; and we have great confidence
that the calculations on which this is grounded are correct*; they
would be brought up by the anticlinal of which the existence has
just been acknowledged. So far then, we may observe, no reason
has been shown why the Survey Section should not be received as
correct.
Prof. Judd’s Section (op. cit. pl. vii..—We do not find any
indications of the direction in which this section is drawn ; but, from
the names of chines which occur in it, we presume that it is intended
to start from Alum Bay in a N.E. direction through Headon Hill,
and after that to follow the coast-line; in this case it is not precisely
comparable with the Survey Section, whose direction is indicated on
the map as passing inland and crossing from sea to Solent. It will be
seen at once why it does not correspond to nature, and agree with
the views of other observers. It will be noticed that the Marine
bed of the Headon Group (3 of fig. 3, pl. vii.) is made to exist at the
sea-level near Widdick Chine; and in the letterpress we read
(op. cit. p. 147) “it is admitted on all hands that at the north-east
angle of Headon Hill the marine band [ Middle Headon beds | makes
its appearence just above the sea-level.” On the contrary, we cannot
imagime any one putting the bed in this position. At the spot indi-
cated the top of the Middle Headon is about 105 feet above the sea-
level; so that the section, in our opinion, is erroneous: the dip
thereby is exaggerated ; and 105 feet of beds are intercalated which
do not exist. We shall prove this presently by a detail-section at
this point of the hill; at the present moment we wish to point out
that, with the correction of this error of 105 feet, the argument
against the accuracy of the Survey section entirely breaks down.
- Thus, we are told that the height of the Bembridge Limestone
above the sea-level at this point is 250 feet (op. ct. p. 147); then,
the marine band being put at the sea-level, it follows that 250 feet
of strata must intervene between that and the Bembridge Limestone ;
“but the Geological Survey [vertical] section shows less than one
half of that thickness of beds, and in Colwell Bay the distance
between the Bembridge Limestone and the marine band is 120
meew yy SS ss But 250 feet of strata is precisely the thickness required
by my interpretation.” Since we have to subtract 105 feet from
* The greater thickness of Upper Bagshot beds above the sea-level in the same
line of section in the old edition of Sheet 47, and in the Plates of the Memoirs,
seems due to the outline of the ground at the S. end being raised too high above
Ordnance datum; probably the accurate height of the Beacon Hill was not
obtainable till 1870, when the revised edition of Sheet 47 was published ; other-
wise the sections are practically identical.
t It would be 133 feet, according to Mr. Bristow’s estimate (Forbes’s Mem.
p. 142), to the top of the Bembridge Limestone in Colwell Bay.
H2
88 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
the estimate in the paper above referred to, we shall certainly have
to abandon this section in favour of that of the Survey; for the
thickness left, viz. 145 feet, more nearly corresponds with the
thickness of the Bembridge, Upper Headon, and Osborne beds, which
are stated by the Survey to exist at this spot, and whose thickness
would be 144 feet *.
It would appear, therefore, that there is no necessity for supposing
“that, in a distance of little more than one mile, a mass of
beds 120 feet thick has expanded to 250 feet, and, further, that the
beds have been entirely changed in their mineral character.”
We do not understand the warning (op. ct. p. 146) against
“trusting to the general impression which is produced by viewing these
beds from a distance,” nor the purport of the following statement :—
“ The strata of How Ledge and Warden Point are seen in such a true-
scale section to be clearly continued in precisely similar beds ap-
pearing underneath the gravel of Headon Hill.” The section offered
to us is on rather too small a scale to show detail ; but, in our opinion,
the beds are inaccurately laid down in Warden Cliff, and no such
bed as the Brockenhurst bed occurs at all in Headon Hill.
Before we commenced drawing our section, we traced the beds
along the cliffs, measured their thickness, and obtained their height
above the sea-level at various points, but found it possible only to
show general results in the horizontal section ; the details are embodied
in the vertical sections.
Vertical Section at North-east Corner of Headon Hill (fig. 1,
p- 91).—We may now proceed to a more detailed account of the
beds. We will begin near the N.E. corner, where the Bembridge
Limestone is seen, indicated on the section (op. cit. pl. vii. fig. 2)
with an asterisk, and lettered 250 feet altitude. (The quarry there
is not now at work; but it is the place at which one of us has ob-
tained most of the finest specimens of Palwothertum which have been
found in the Isle of Wight.) We take the thickness from the
Survey Memoir as 25 feet.
Beneath this, in the section (fig. 3, pl. vil.), we notice a blank
space with the legend “slopes covered by gravel and landslips.”
We think this scarcely a correct description. Landslips exist in that
the clays and marls tumble and form taluses ; but we saw no gravel
covering the slopes between the Bembridge Limestone and Widdick
Chine ; nor indeed does it entirely conceal the beds between the
Bembridgeand Upper Headon Limestones all the way to Heatherwood
Point in the other direction; at intervals tumbled gravel conceals
a limited portion of them.
The gravel west of Widdick Chine is not accurately depicted: the
thickness is exaggerated, while its horizontal extent is overestimated
here t. It does not appear in the cliff certainly beyond 80 yards
* Taking the Bembridge Limestone at 25 feet, the Upper Headon and
Osborne at 119 feet, as read off their vertical section by scale, after altering
their lower boundary a few feet to correspond with our own.
t Mr. Bristow (Forbes’s Mem. p. 105) gives the entire horizontal extension
of the Lacustrine beds (Post-Tertiary) on both sides of the chine as 350 yards ;
the section under review makes the gravel extend about 720 yards.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 89
from the chine on the west side (private grounds interfere with
examination nearer the chine).
We should say, from our examination of the ground which inter-
venes between the escarpment of the thick Upper Headon Limestone
and the Bembridge, that there is no difficulty in seeing what beds exist
there. It is true they are sufficiently interrupted by local taluses to
cause trouble in making a continuous measurement ; but the tumbled
portions are partial and affect only a few feet of beds at a time, so
that by moving the observer’s position laterally it is possible to see
all the bedsinturn. ‘This we claim to have done; we do not pretend
that our measurement of the beds is any thing but rough, though
controlled by repetition, because we had no levelling-instruments with
us, and in shitting horizontally from one spot to another there might
be frequently a slight error in picking up the next bed to be
measured. We might describe the beds immediately below the Bem-
bridge Limestone, in descending order, as follows:—yellowish and
ochry marls, red and grey mottled marls, marly clays with nodular
bands, greenish-grey clays, pale greyish clays, grey and ochry clays,
stiff pale or whitish clays with calcareous lenticular bands, red and
green mottled marls, ‘“ cherry marl” with calcareous bands. These
are the Osborne beds of the Survey ; and they come in the precise
position assigned to them in the Survey Memoirs. They are well
characterized by the ‘cherry marl”—the mottled red and pale
greenish marl which distinguishes the group from the Upper
Headon ; and we consider the subdivision a very useful one in the
classification of beds. Their thickness here, by our comparatively
rough way of measurement, is 70 feet. The vertical section of the
Survey Sheet 25 gives 71 feet, reading off by scale down to the bed
which we have taken as our boundary; their measurement seems to
have been taken near Heatherwood Point, where this series contains
a thick limestone of 18 feet; as noticed by previous observers, this
limestone thins out to the east, and is only represented by nodular
calcareous bands at the east end of the hill ; its loss will probably be
compensated by an increase in the clays. Our results are perhaps suffi-
ciently near to those of the Survey to prove that the same series of
beds has been examined in both cases. Weshould remark that from
the lower red beds it is perfectly easy to draw a continuous vertical
section to the beds below; and from here our measurements to the
Lower Headon are uninterrupted in a vertical line. The Osborne
beds yield few interesting fossils; Lomnea is abundant in the
calcareous bands ; but, as noticed by Forbes (Mem. p. 81), the shell-
substance is not preserved. These beds are identical lithologically
with the mottled red and pale green series at Cliff End.
The beds next below the red series are grey and ochry clays, very
rich in Potamomya gregaria and Paludina lenta beautifully pre-
served: we place these in the Upper Headon; they are about 15
feet thick *.
* Tn the Survey Section no. 5, at Headon Hill (sheet 25, Vert. Sect.), these
clays are included in the Osborne series; but in the Vert. Section. no. 4, at Col-
rh the boundary is so drawn that analogous claysare put into the Upper
Headon.
90 ON THE BEDS AT HEADON HILL AND COLWELL BAY.
This brings us to the vertical escarpment of the thick limestones,
so conspicuous a band along Headon Hill cliffs that it is indicated
on the Ordnance maps, both on the 25-inch and the 6-inch. We
pause awhile to draw attention to the fact that we have accounted
for about 110 feet of beds from the top of the Bembridge to the top
of the great limestone (Upper Headon) ; and the Brockenhurst series
does not exist here. There is not a single marine fossil to be found
am that interval; nor is there any bed with the faintest resemblance
either lithologically or palceeontologically to the Colwell-Bay Venus-bed.
This is in opposition to the view (I. ¢. p. 176 e¢ passim) that the
Colwell-Bay series exists here “‘entirely concealed” by some supposed
gravel talus*; yetit is upon the existence of such a second marine series,
thus supposed to be added above the Venus-bed that the presence of
a Brockenhurst series at the west end of the island is inferred.
Next we turn to consider the thick limestone of the escarpment,
the Limneea-limestone of the Upper Headon. It is in several beds,
of which details are given by the Survey; we measured it by sus-
pending a tape, and found it 27 feet (fig. 1, p. 91).
The only difficulty in correlating the Headon-Hill beds with those
of Colwell Bay is centred in this limestone: it might be a difficulty
to those who would have expected a priori that the limestone would
have maintained its thickness in direction of dip for a mile or two
to the north; for we identify it with a limestone at Cliff End not
above 1 foot 8 inches thick. It would be equally a difficulty aecor-
ding to the correlation which identifies it with the How-lLedge
limestone (op. cit. p. 144); im this case the 27 feet has thinned to
3 feet at How Ledge, a distance of 14 mile in a straight line, while
in Warden Cliff (only 926 yards distant from the Headon-Hill bed)
it is about 5 feet; so that it must have thinned very rapidly at the
first stage. The limestone in the Upper Headon at Cliff End, with
which we identify it, is distant 1 mile 926 yards. In either case it
thins out considerably to the north, as noticed by E. Forbes (Mem.
p. 84). We shall be able to prove that it does not occupy the same
position as the How-Ledge bed; for we have recognized that bed,
which forms the summit of the Lower Headon, at a lower position
in Headon Hill and in its natural position, viz. below the marine
series (Middle Headon), as in Warden Cliff, where it was last seen.
As a paleontological distinction between the Upper Headon limestone
of Headon Hill and Cliff End + and the Lower Headon limestone
* With respect to the “inextricable difficulties and confusion” (7. ¢. p. 144)
in which the Survey is supposed to be involved by their not allowing the Col-
well Marine bed to come where the Osborne beds are placed, and which is sup-
posed to be shown by 48 feet of strata being classified in the letterpress (Forbes’s
Mem. p. 81) as Osborne, while in the plate they are classed as Upper Headon,
this is merely a, question of classification and the drawing of a boundary-line,
matters entirely subjective and not affecting the total thickness ; their vertical
section shows almost the same thickness of beds consistently, notwithstanding
certain irregularities in the boundaries and classification.
t In the legend to the Survey Vertical Section, sheet 25, no. 4, this limestone
in the Upper Headon is said to form How Ledge; this is plainly an oversight
or clerical error, as is also the statement in Forbes’s Memoir, p. 132, that the
How-Ledge bed is faulted in Warden Cliff. The fourteen faults mentioned affect
the Upper Headon limestone at Cliff End: their section is fairly correct; but
there seems to have been some confusion between Warden Point and Cliff-Hnd
Point in the letterpress.
Fig. 1.— Vertical Section of Beds at the North-east corner of Headon Hill.
63-8 0
UppEerR HEADON.
bs
oOo
® 8
9 in.-2ft
6 in
6 in
ft." 1m:
1 10
MIDDLE HEADON.
~~ A
ow
f=)
seen.
LowER HEADON.
CO
for)
(Scale, 8 feet to the inch.)
BEMBRIDGE LIMESTONE ...... a0 feet.
OSBORNE BEDS
SO esac r esos ersorccras
WPPER HIBADON ....0:0.0-0s00008 9 a (total).
al
& aye 36
CO
Part of thick Limnea-limestone. Limnea fusiformis, &c.
Laminated greenish clay, with broken Paludina.
Whity-brown to buff sands, with layers of lignitic matter.
Greyer sands below. Potamomya, Melania muricata, Unio, Paludina lenta.
> Lignite.
* Greyish-green oye. C. ven- \ Vicarya concava, Marginella vittata, Neri-
tricosum-bed With ...........026 tina concava, Melania muricata, &e.
--- Limnea-limestone, soft and crumbling, with a thin lignite at top.
-*-Verdigris-green clay, with rootlets.
Limnea-limestone.
Stiff green clays with conchoidal fracture in drying.
Oyster-bed towards the base.
Fusus labiatus, Mel. fasciata, M. muricata,
Clay becoming greyer below. ) Nerita aperta, Cer. variabile, C. pseudo-
IM OSSIUS |i cccestcseerstessseccceees cinctum, Ostrea velata, Mytilus affinis, Cor-
bicula obovata, Lucina colvellensis.
Alternating grey and ochry clays.
Cyth. incrassata, Mactra fastigiata,
“‘ Venus-bed,” richest portion, con- Mya angustata, Corbicula obovata,
tains scattered flints, brown sandy | Wucula lissa, N. headonensis, Trig.
- clay becoming green clay and sand deltoidea, Fusus labiatus, Cancell.
Ibelow-m Ue ROSSILSSscsceseccs-0s.-sanenescess elongata, Melanopsis fusiformis,
/ Voluta spinosa, Vic. concava, Natica
Thin grey sandy clays, Studert.
weathering brown.
Cytherea incrassata &c. scattered throughout.
Mya angustata, especially near base.
Trig. deltoidea, Cer. pseudocinctum,
Chocolate-brown or blackish sands. { Natica labellata, Melan. fusiformis,
Trigonocelia-bed.
Blackish-brown sands, Weritina-bed: WV. concava, M. fusiformis, C. obovata.
Very stiff tenacious clay.
Limnea-limestone, ‘‘ How-Ledge limestone:” ZL. longiscata, fusiformis, &c.
Whity-brown or yellow sands and sand-rock, with layers of Paludina and
Potamomya.
[The base concealed by tumble and undercliff. |
92 H, KEEPING AND E. B. TAWNEY ON THE BEDS AT
of How Ledge, we may adduce that the former is very rich in
Planorbis, while in the latter- these shells are comparatively rare,
the fossils being chiefly Limnea.
As the Upper Headon limestone is the strongest bed in the
section and forms an escarpment through the greater part of Headon
Hill, in it we may obtain a datum line. We take as a point of
reference the spot where the top of the escarpment cuts the surface
of the ground or outline of the cliff; this 1s seen on the 6-inch or
25-inch map to be about halfway between the 100 feet and 200 feet
contour-lines. From these points of known altitude, by the aid of
the barometer, we obtain the height of our point of reference: ibis
about 140 feet above Ordnance datum.
The beds below the Limnea-lmestone are green clay, 1 foot,
with broken Paludina, then pale butt or whitish sands, varying from
63 to 8 feet, with occasional layers of lignitic matter, Potamomya,
and Melana muricata; below, where it is sometimes grey, Unio
Solandri and Paludina lenta may occur. We take this bed with
the 3-inch lignite below as the base of the Upper Headon. The
boundary chosen is, of course, arbitrary ; but the fact of the next
bed being decidedly brackish inclines us to draw the division from
the Middle Headon here ; the Survey vertical section, sheet 25, places
it a few feet lower.
Our estimate for the Upper’ Headon at Headon Hill amounts to
a thickness of 50 feet; the thickness on the Survey vertical section
is given as 37 feet ; but if we read off the distance between the beds
which we have taken as boundaries, it becomes 48 feet. The com-
bined thickness of Osborne and Upper Headon beds, according to
the Survey section, is 119 feet, 2.¢. adopting the top of the C. ven-
tricosum bed as the boundary ; our estimate, taken at the north-east
end of the hill, is 120 feet. The agreement is sufficiently close to
render it probable that a thickness above the average of the cal-
careous portion is accompanied at the same spot by a diminution in
the clays; so that the balance of average thickness is maintained at
both ends of the hill. As we have said, we think it convenient to
retain the name “ Osborne Series ” for the red and greenish mottled
clays and marls and pale greenish-white limestones, since these
‘physical characters distinguish them at once along this side of the
Solent. We must decline to accept the statement (op. cit. p. 169) that
‘‘under this name beds lying below the Brockenhurst series, as at
Headon Hill, have been confounded with others on a totally diffe-
rent horizon, above the Brockenhurst series.”
We next come to the Middle Headon. HH. Forbes relates (Mem.
p. 85) that the uppermost and lower portions at Headon Hill are
brackish-water beds abounding in Cerithium ventricosum, C. pseudo-
cinctum, C. concavum, Neritina concava, and Nemature, the condi-
tions being less purely marine than at Colwell Bay. This is, no
doubt, true of the series as a whole ; for below the C. ventricosum bed
there are two freshwater Limnea-limestones. But it appears to us
that too much has been made of this ; for instance, the lower Neri-
tina-bed is identical in Headon Hill with the similar bed at Warden
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 93
Cliff, and again in Colwell Bay, both physically and as to its fossils ;
when we come to the portion of the series richest in Cytherea incras-
sata known as the ‘“ Venus-bed” proper, we find identically the
same fossils as in Colwell Bay; we cannot detect any difference, so
far as our researches go.
The uppermost bed is dark greenish clay, varying from 9 inches
to 2 feet in thickness. When at its thickest the sands above are
proportionally thinner. It is extraordinarily rich in fossils for the
depth of one foot, chiefly Meritena concava, Cerithium (Viearya)
concavum, C. ventricosum, Corbicula obovata, Marginella vittata,
Melania muricata, Melanopsis fusiformis. We may callit the C. ven-
tricosum bed; for this fossil seems almost confined to this horizon,
while the Vicarya concava is found here all through the Middle
Headon, though especially plentiful in this bed; its underside is
occupied by an impure lignite band, with freshwater shells (Limnea
and Planorbis), and rootlets, lying on a thin crumbly buff Limnza-
limestone. Both together are 4 to 6 inches. Below is verdigris-
green clay, 6 inches; next a buff freshwater limestone with Limnea,
1 foot 8 inches to 2 feet, the shells frequently blackish in colour.
These beds betoken certainly a recurrence of freshwater conditions
after the brackish bed above. Next follow truly marine beds—first
stiff green and grey clay, about 9 feet, with a conchoidal fracture
when dry. ‘The abundance of oysters, O. velata (Wood), is the chief
fossil feature ; these and the other fossils occur mostly towards the
base. Such fossils are Musws (Pisania) labiatus, Nerita aperta, Me-
lana fasciata, M. muricata, Cerithiwm variabile, C. pseudocinctum,
Mytilus affinis, Corbicula obovata.
The fossils cited are merely the most common, such as may be
found in a few minutes’ search; but these being the most charac-
teristic, seem to us precisely those required for the identification
and correlation of beds.
Comparing the beds noticed so far with those at Colwell Bay,
we observe practically identity of fossils; this last, which we may
call the oyster-bed, is identical with the oyster-bed of Colwell Bay ;
in both localities OC. ventricoswm occurs above this bed, and there
only, so far as we know.
Next below follow alternations of grey and ochry silts, 3 feet, in
which we observed no fossils. Below are 11 feet of beds, brown
sandy clay above becoming green clayey sands below, and then grey
sandy clays: this is the ‘ Venus-bed ” of collectors ; Cytherea imcras-
sata occurs near the top and is scattered throughout the whole bed,
but is most abundant for the space of one foot. The fossils obtained
from the Venus-bed in a few minutes’ search were Cytherea incras-
sata, Mya angustata, Mactra fastiqiata, Psammobia rudis, P. westu-
arina (Hid. MS8.), Nucula headonensis, N. nudata, Trigonocelia del-
tordea, Corbicula obovata, Vicarya concava, Ancillaria buccinordes,
FPusus labiatus, Cancellaria elongata, Natica Studeri, N. labellata,
Voluta spinosa, Melanopsis fusiformis, Nematura parvula, Limnea
longiscata, Planorbis obtusus, crab-claw (Callianassa), coprolite.
94 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
Towards the base Mya angustata and Corbicula obovata were parti-
cularly abundant.
Next below the Venus-bed is the Trigonocelia-bed, chocolate-
brown sands, 34 feet, with sometimes a blackish tint ; we so call the
bed from the principal fossil which occurs at precisely the same
horizon in Warden Cliff and Colwell Bay; other fossils are Ceri-
Ehium pseudocinctum, Melanopsis fusiformis, Natica labellata. Below
are blackish-brown sands, 6 inches; at base is enough carbonaceous
matter almost to amount to a lignite band; this may be called the
Neritina-bed, the chief fossils are Weritina concava, Melanopsis fust-
formis, Corbicula obovata, the latter in perfect condition, very large,
and showing concentric colour-bands. The Nertina-bed occurs in
the same position towards the base of the series in Warden Cliff
and Colwell Bay. This can only be explained by admitting that
the marine series in Totland Bay and Colwell Bay are identical ;
the Ventricosum bed at the top, and the Neritina and Trigonocela
beds at the base, identical in physical and fossil characters, are
strong presumptive proof of this.
Below is very stiff dark-grey clay, 1 foot to 1 foot 3 inches;
fossils occur in patches, Neritina concava, Cerithium pseudocinctum,
Melana muricata, Limnea, Corbicula obovata. This is the lowest
bed of the Middle Headon here. Summing up, we obtain a thickness
of from 31 feet 9 inches to 33 feet for the Middle Headon of Headon
Hill at the N.E. end. Reading off the Survey vertical section by
scale, we obtain 35 feet for it between the boundaries adopted by
us * for the thickness towards the west end.
The height of the base of the Middle Headon above the sea at
this point, viz. about 120 yards in horizontal distance west of our
reference-point, is by subtraction 72 feet. Direct barometric obser-
vations gave about 70 feet. We have already used these figures
when alluding to the position assigned to this series.
The first bed of the Lower Headon is a Limnea-limestone of the
usual buff colour: it is 2 feet thick at this point; but a little further
west we obtained a measure of 4 feet. This is in our opinion the
well-known bed which forms the top of the Lower Headon in Warden
Clif, where it is quite a marked feature. It has there and in Col-
well Bay precisely the same position in the series, supporting the
Middle Headon—recognized by the Neritina-bed with all its charac-
teristic features, the Trigonocelia-bed, and so on. From Warden
Cliffit is traceable uninterruptedly to How Ledge, where it disappears
beneath the sea-level ; we therefore speak of it as the ‘“‘ How-Ledge
limestone.” It is correctly drawn on the Survey vertical sections,
sheet 25, nos. 4 and 5, where in the legend is a clerical error, to
which we have already alluded. This bed is so distinctly lacustrine,
* Some irregularity in the boundaries of the Survey vertical section is to be
noticed : viz. in the Headon-Hill Section, no. 5, the boundary is placed below
the How-Ledge Limestone ; in the Colwell-Bay section, no. 4, the boundary is
placed at one bed above the How-Ledge Limestone; this seems an error of the
engraver, and of course does not affect the thickness of the beds.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 95
being almost made up of Limnea shells and their débris, that. it
seems most convenient to include it in the Lower freshwater group ;
and it makes an especially good boundary.
The beds which follow next below the Limnza-limestone at this
spot are whity-brown or yellowish sands, and sand rock with
Paludina and Potamomya in layers ; 8} feet are seen; this is all
that is exposed of the Lower Headon here. At this spot all the
eround below is tumble or undercliff; and for a more complete
section of the Lower Headon in the present state of the cliffs we
shall do best to take the one exposed in Warden Cliff and under
Totland Bay Hotel, where the fresh road-cuttings to the New Pier
have been of service to us.
We consider that we have already sufficiently proved the identity
of this lower limestone in Headon Hill with the How-Ledge bed of
Warden Cliff; but if any objection be raised that its relations to
certain specified bands in the (Middle Headon) Marine series being
found identical in both localities is not conclusive—even though it
has been shown that no other marine bed exists in Headon Hill—
we have further means at our command. ‘There are, however, only
two beds in Headon Hill with which the How-Ledge bed could be
continuous: viz. either it is the same as the thick Upper Headon
limestone (which we consider impossible, as the beds both above and
below would then just be reversed, viz. freshwater above and marine
below, instead of vice versa), or it must be identical with the one to
which we assign it. It is possible, however, to settle the point by
ocular demonstration*. Though the How-Ledge limestone is
denuded from the top of the curve between Weston and Widdick
Chines, some of the lower beds are traceable the whole way. Ac-
cordingly we can join on the section in Headon Hill to that in
Warden Cliff. We account thus for a continuous section of beds
from the lowest seen beds of the Lower Headon, through the Middle
and Upper Headon of Colwell Bay, to the Bembridge Limestone on
the north, and again from the same base of the Lower Headon,
through the succeeding Lower Headon beds in the cliffs between
Weston and Widdick Chines, to the sand below the How-Ledge
limestone at the N.E. corner of Headon Hill, and thence up to the
Bembridge limestone on the south ; and we find that the section is
identical in both cases. There is only one Marine (Middle Headon) |
series, lying between two freshwater ‘series, the Lower and Upper
Headon.
Of course, all this has been done before by the Geological Survey,
and our work is nothing but a confirmation of results already suffi-
ciently established by E. Forbes and Mr. Bristow.
On our horizontal section of the coast we have endeavoured ‘to
represent the position of the beds in the cliffs and the extent to which
* We are indebted to the Rev. O. Fisher, F.G.S., who specially visited Tot-
land Bay this autumn, for the information that the Venus-bed is found in the
Totland-Bay brickyard some little way above and behind the top of the cliff
between the chines. He points out that since this is the only part where it is
missing from the cliff, itis the link needed to prove that the bed is continuous
all through.
96 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
they are traceable ; but though the vertical scale is more than twice
the horizontal, it is not possible to show the details; for these
we must refer to the vertical sections.
Lower Headon Beds of the cliffs between Weston and Wraddick
Chines.—We left off with the Potamomya-sands, 83 feet below the
How-Ledge limestone ; these are easily traceable through the grass-
slopes, exposures of a few feet occurring at intervals all the way to
Widdick Chine, about 230 yards distant. There good sections are
seen on each side of the roadway; here the sands have in the upper
part more clay mixed with them, as in Warden Cliff. Whiter sands
are below; above are alternating whity-brown sands with bluish
silts. Melania turritissima occurs in the latter, a shell which occurs,
indeed, in the Bembridge Marls at Hamstead, but which, in this
district, we only know at one horizon, viz. the Unio Solandri bed,
and one above that, at Warden Cliff and Colwell Bay; we remark
its analogous position at Widdick Chine. Below the sands, again, is
pale greenish clay, 3 inches ; in descending order, soft buft Limnea-
limestone, 1 foot; brownish sands with Potamomya and reptile
dermal ossifications : these occupy the position of the Crocodile-beds
in the Lower Headon at Hordwell; they continue along the cliff as
we walk northwards. Below is a carbonaceous band or impure lig-
nite, 6 inches, then a repetition of clays with carbonaceous layers, fol-
lowed by another Limnza-limestone, 10 inches, Potamomya-clays,
4 feet, another Limnea-limestone, 1 foot, greenish clays with Palu-
dina lenta, Potamomya plana, Melanopsis brevis, Limnea &e. ;
another Limneea-limestone, 8 inches, full of Gyrogonites, below that
clay with carbonaceous layers passing to drab sands, about 2 feet ;
then a lignite layer and impure Limnea-limestone, soft and crumbling
at the outcrop. The limestone full of Gyrogonites is noteworthy, as
it occurs only low down in the Lower Headon, and serves to mark
our position in the series at this spot. Now this Chara-limestone is
exposed again at the back of the Reading Rooms, where there are |
the same five limestones seen as near Widdick Chine, the Chara-bed
being the lowest but one; this is well seen behind the Reading
ltooms, where there has been a cutting through the Lower Headon
beds for a new pathway. It will be noticed that we have passed
five thin Limnea-limestones in the lower part of the Lower Headon
in the cliffs immediately north of Widdick Chine, and again behind
the Reading Rooms; we see them again as they rise from beneath
the sea-level beyond the new pier under Warden Cliff; they are
seen also in the recent scarping under Totland Bay Hotel. The
continuity, then, of the section from the five lower limestones under
Warden Cliff through Weston Chine to Widdick Chine is undoubted ;
and from there we continue through the sands above to the How-
Ledge limestone in Headon Hill. The beds in the cliff here belong
entirely to the Lower Headon*.
* The top of the cliff at the back of the Reading Rooms has a capping
of about 7 feet of Post-tertiary sand ; at the base of this is a layer of flints and
derived marine fossils, Cytherea incrassata, Ostrea velata, &e., showing that
the marine Middle Headon series existed here above this level. This Post-
tertiary sand lies on the (Lower Headon) Warden sands.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 97
Lower Headon of Warden Cliff.—The lowest beds seen are below
the Totland Bay Hotel at Weston Chine. We therefore start from
here in making a measure of the Lower Headon series, meeting higher
beds as we go north towards Warden Point. ‘The details of this
measurement are given in the vertical section, fig. 2(p. 98); we need
here allude to only a few of the beds. The lowest bed seen in
Totland Bay is a few yards south of the Coast-guard boathouse ;
here are visible, in ascending order, whity-brown sands, 13 foot, a
hard purple sandy ironstone, 6 inches, greenish clay, 4 feet.
In our vertical section, fig.2, we have drawn an interruption in these
clays, because we are not absolutely sure that they are identical with
the similar clay in the road-cutting at the pier-head on the other
side of the boathouse; there is little doubt of it, however. At the
pier-head are seen 3 feet of clay in the road-cutting (after our
section was drawn, on a later visit, a drain-opening showed 41 feet) ;
and from this point the section 1s continuous without interruption.
There is therefore only a possibility of error of a few feet.
Five thin Limnea-limestones will be noticed. The two lowest
contain Chara-seeds at the pier-head; on following them to their
outcrop along the shore it is found that the fourth of them also
has Chara-seeds at that point; the fifth, 1 foot 3 inches thick, is
50 feet. below the top of the How-Ledge limestone, or top of the
Lower Headon.
From the top of the cliffs these limestones may be seen at low
water, forming five submarine ledges parallel to the great ledge at
Warden Point; they strike N. 36° W.
As there is great uniformity in these freshwater beds, and their
fossils mostly occur in the Upper Headon also, we pass over many beds
to notice the sand-rock bed, which is a conspicuous feature in Warden
Chiff. This sandstone, somewhat calcareous at places and friable at
others, forms Warden Ledge, and runs out at the top of the cliff
_close below the flagstaff of the coast-guard station.
About 11 feet above that comes the Unio Solandri bed* with
Melama turritissema, a bed of which we have already noted a portion
in the cliff at Widdick Chine; the MW. turritissima occurs through
a greater thickness of the 114 feet of clays than does the Unio.
Next comes the How-Ledge limestone, 5 feet, in two beds containing
Limnea fusiformis, with a carbonaceous or lignitic band at the base.
The shells are more crowded at the base; and the lower surface of
the blocks fallen from the cliff is a sight pleasing to the collector
of fossils. The dip of this bed in Warden Cliff, calculated from its
horizontal extension on the 25-inch map, between its position at How
Ledge at sea-level and a point of known elevation near the flag-
staff, is a slope of about 1 im 45. This How-Ledge bed crops out at
the top of the cliff, a little north of the coast-guard flagstaff; it is
* 'The Unio-bed with Melania turritissima occupies an analogous position at
Hordwell Cliff, being at about the same distance below the Lymnza-limestone
(which is a diminutive representative of the How-Ledge bed), where it has pre-
cisely the same lithological characters with the same abundance of black seeds
(Carpolithes) as at Colwell Bay and Warden Cliff; it crops out again with the
same fossils on the shore immediately south of Milford.
98 H. KEEPING AND E. B, TAWNEY ON THE BEDS AT
Fig. 2.—Vertical Section of Lower-Headon (freshwater) Beds eaposed
between Weston Chine and Warden Cliff.
(Scale, 12 feet to the inch.)
Limnea-limestone, in two beds, buff colour.
How-Ledge bed; extends from How Ledge to Coast-guard
Station.—Z. fusiformis.
= Lignitic or carbonaceous band.
Pale grey clays, rather mottled. Paludina at intervals.
but more so above. WMelania turritissima and other fos-
{batons greenish and greyer clays, rather sandy below,
sils in layers at intervals,
Unio-bed.
Laminated grey sandy clay, with Unio Solandri, Mel. turritissima.
Stiff clays, grey or brown in places,
=| Sandy grey clay, more sandy above, with Paludina lenta, Mela-
nopsis brevis, Potamomya plana, Unio Solandrt.
>:| Pale whity-brown crumbling sand-rock, - .
‘| with strings of clay. } Cyr ena depen
| Ferruginous sand-rock, variable in thickness, with Limnea, &e.
Concretionary calcareous sand-
rock, | 7;
forms Warden Ledge. } wer alp BMSEIOCIL LG:
LowER HEADON.
eee
on _ bo bo lor} ler) oO nn =
(S) (=) Ne) (>) (=) fer) (=) =) =
White and whity-brown sands, Potamomya in layers at intervals.
10 0
20 Stiff grey or sandy clay, with Potamomya crowded together.
=, Lignitic band.
S150 Greenish clay. Potamomya gregaria.
1 3 Buff-coloured limestone, with Limnea.
Lignitic or carbonaceous band.
33-4 0 = Greenish-grey clays.
0 6 Soft crumbling buff limestone, with Limnea longiscata.
Grey marly clay.
2 0
0 8 ==| Bulf limestones, with Limnea.
50 SS Greenish clay.
[bed.
= Buff compact limestone, with Chara-seeds (Gyrogonites) Chara-
2:27] Whity-brown sand-rock, with lignitic band below.
“| ,..Butt limestone, with a few Chara-seeds.
-*-Carbonaceous layers.
Green clay (behind wall at Pier-head).
...Green clay, a little south of Coast-guard boathouse.
=| ---Nodular purple-red ironstone band.
<| Pale yellowish or whity-brown sands.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 99
denuded away in the centre of Totland Bay. It cannot, however,
have been many feet above the present cliffs near Widdick Chine,
while a little south of that it exists in the cliff. At the N.E. corner
of Headon Hill we noted it at a height of 70 feet above the sea ; it
is well seen also in the cliffs near Heatherwood Point, where it has
a somewhat higher elevation.
There is evidence of an anticlinal in Totland Bay, as indicated in
K. Forbes’s sketchy diagram ; the summit of the anticlinal we infer
to be near the old wooden pier.
If we add up, we obtain a thickness for the Lower Headon exposed
in Warden Chiff of 714 feet (supposing no interruption at the point
specified above). It remains to settle the relation of the lowest bed
here seen to the Upper Bagshot Sands.
The junction of the Lower Headon with the Upper Bagshot is well
seen north of Alum-Bay Chine; immediately above the Upper Bagshot
sands come greenish-grey clays ; then, in ascending order, alternation
of clays and sands ; next, pale greenish-grey sands ; then a stiff marly
clay: total 16 feet. Above is a purplish red clay-ironstone band;
and succeeding that is the first thin Limnea-limestone.
If we consider this red iron-band to be at the same horizon as
that noticed under Weston Chine, as is extremely probable (though
it is some 4 feet nearer to the lowest Limnza-limestone), then we
must add 12 or 16 feet to the 71 feet obtained for the Lower Headon
in Warden Cliff, making a total of 83 or 87 feet before we reach the
yellowish sand of the Upper Bagshot.
Knowing now the full thickness of the Lower Headon, we are
able to test the argument as to the position of the Upper Bagshot, or
Headon sands, as they were once called by E. Forbes (Mem. p. 34-6),
in Totland Bay. It is stated (op. at. p. 147) that the Survey
actually represent these as occurring, in both the Vertical and Hori-
zontal Sections, near the summit of the anticlinal in Totland Bay*.
There seems a little inconsistency in the Survey Vertical Sections
concerning both boundaries of the Lower Headon; if we may classify
these green clays in the Lower Headon, and then read off by scale from
the top of the How-Ledge bed, the Survey Section would give a thick-
ness of 85 ft. for the Lower Headon in Totland Bay.
It is urged “that the Headon-Hill sands do not occur in the
position indicated by the Geological Survey ;” and the crucial test of
* We pointed out above that the Survey Vertical Section [edition 1870] shows
them only just above the sea-level at a point some way inland. The Vertical
Section we are inclined to interpret in this way—that the beds denoted Upper
Bagshot in Totland Bay are what we have classed in the Lower Headon ; for the
legend states, below the “‘clay-ironstone ” are 6 inches sand in “ Totland Bay,”
then “ green clay with lenticular patches of sand” 15 feet, so that the de-
scription agrees fairly with our lowest bedsat Heatherwood Point. The Survey
Section does not state that these were exposed in the centre of Totland Bay; but
as Heatherwood Point is the western point of the bay, we may assume that
they may have been seen anywhere short of that point along the base of Headon
Hill, where it is quite certain that they exist, and must have been open at that
time at more points than one; for the white glass-house sands were then being
actively worked in Headon Hill, and the yellower sands above them may still
be seen about a mile from the N.E. corner of Headon Hill.
100 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
the excavations at the new Reading Rooms is supposed to prove
“‘ that beds are [there] found which have their exact counterpart in
the Headon-Hill section, not at the base, but at a much higher part
of the series.” We can readily understand that the Upper Bagshot
sands were not found in the excavation; we could even have
predicted the fact beforehand ; from a rough calculation, we estimate
that the sands are above a dozen feet below the foundation. In
favour of this view, we may add that, when the old wooden pier was
being made, one of us heard from those engaged in the work, that
the piles were driven with difficulty because of their piercing solid
sand! *,
But putting aside the question as to their exact depth here below
the Reading Rooms, we are able to refute the notion that any thing
higher than Lower Headon beds exist here. As mentioned above, we
recognized immediately behind the Reading Rooms the five Lymnea-
limestones which come below the Potamomya-sand, both at Widdick
Chine on the south, and Weston Chine on the north, between which
places the sands may be traced almost continuously. The whole of the
cliffs between Weston and Widdick Chines are occupied solely and
throughout by Lower Headon beds (neglecting the cap of Post-
tertiaries). All this part of the section (op. ct. pl. vu. f. 2) is in-
accurate, in consequence of the Middle Headon being placed too low
in Headon Hill.
Middle Headon of Warden Cliff—Again, we cannot agree with
that part of the section between Weston Chine and Warden Point.
Here no marine bed is indicated ; for in fig. 3, the section drawn to
true scale, the Colwell bed is made to die out before the Warden
battery is reached, which is occupied by an exaggerated thickness of
gravel 7.
There is no fact more patent to any observer than that the Col-
well-Bay marine bed extends all through Warden Point and Cliff,
where it is supported by the How-Ledge limestone. We made a
measure in detail of the Colwell marine bed (Middle Headon) at a
point about midway between Warden Battery and Weston Chine ; it
is here 344 feet thick ; we noticed there the Neritina-bed + with its
characteristic features and fossils below the Venus-bed as at Col-
well Bay and Headon Hill. It would be wearisome to give all the
details ; but the Colwell bed here is easily recognizable as identical
with the Middle Headon of Headon Hill, both physically and pale-
ontologically. At Warden Battery, above the Middle Headon, comes
some Upper Headon § besides the Post-tertiary cap.
In the section drawn to true scale (pl. vu. fig. 3) the Colwell-
Bay marine bed has its horizontal extension curtailed by almost one
* The iron columns of the new pier are stated to pierce a bluish clay; we
should interpret this to indicate the clays immediately above the Upper Bagshot
Sands, and which are described as greenish in the Survey section.
t We cannot reconcile this with fig. 2 of the same plate, where the marine
bed is more nearly correctly drawn.
{ Previously noted as bed 16 by Dr. Wright, Proc. Cotsw. Club, i. p. 95, and
Ann. & Mag. Nat. Hist. s. 2, vol. vii.
§ Described by Dr. Wright in 1850 as bed 5, Proc. Cotsw. Club, i. p. 90.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 101
half; the result is that the dip is considerably exaggerated. Again,
in Headon Hill an exaggeration of dip is produced by the error of
105 ft. in plotting the marine beds. 'The effect is that the identical bed
(Middle Headon) is split into two beds separated by 120 ft. of beds.
From our point of view this could only be done by counting more
than 100 ft. of beds twice over. In the legend attached to the diagram
section fig. 2, “‘ new interpretation,” the beds g are, in our opinion,
the Lower Headon; f is the Middle Headon ; e the Upper Headon ;
d and ¢ are the Lower Headon; 6} is the Middle Headon again.
According to the old view, which we certainly should prefer, this last
105 ft. has no existence in fact*.
Lower Headon of Colwell Bay.—The section in Colwell Bay is
continuous with that of Warden Cliff; but in the bay, as we go
north, a few lithological changes occur in the marine beds 7, as
noticed below, and which cause the marine beds at one part of Col-
well Bay to differ far more from the same beds at the centre of the
bay than the latter do from the marine beds of Headon Hill. On
rounding Warden Point, beyond the sea-wall, is a small rifle-target ;
and from here the beds are fairly well exposed throughout the bay,
though tumbled portions or a diminutive undercliff may conceal
some of the beds in places, sufficiently to give considerable trouble
in measuring the beds. °
The Unio-Solandri bed with Melania turritissima has been fre-
quently worked by one of us below the How-Ledge limestone here
but this summer we could only find tumbled portions of it. The said
limestone rises from beneath the sea-level at How Ledge +, whence
its appellation, and crosses Colwell Chine; here and at the target it
has the same lignitic band and clays beneath it as on the south side
of Warden Cliff; it thins down to 8 ft. north of the chine. We
mention these upper beds of the Lower Headon to show that the
Colwell-Bay marine bed, as at Warden Cliff, reposes on the same
succession of beds as in Headon Hill.
Middle Headon of Colwell Bay.—The lowest or Neritina-bed at
the S.W. end of the bay, by the target, is now covered by tumbled
matter, but is well seen a little further on about 50 yards short of
Colwell Chine. Here, 7. ¢. between the target and the chine in the
* The diagram in Forbes’s posthumous work is so schematic that it omits
the higher part of Headon Hill, and, perhaps for clearness sake, the effect of
the anticlinal is exaggerated. It is rather severe to treat it as if it were drawn
to scale, and, because the Upper Bagshot Sands were brought up too much in
the centre of the roll, to say that H. Forbes was “‘mistaken in his interpretation”
(op. cit. p. 176) of the beds. Forbes’s diagram, in fact, with this qualification,
represents the beds in their right position ; thus the Lower Headon, no. 6, occu-
pies the summit of the cliffs in the centre of Totland Bay, while no. 7, Middle
Headon, is denuded from above it—all which is perfectly correct.
Tt Since Warden Battery has been built it is forbidden to search for fossils
on the slopes at Warden Poimt. Many years ago one of the authors was in the
habit of frequently exploiting the beds here for fossils, and many of them are
incidentally described by Dr. Wright, Proc. Cotsw. Club, i. pp. 91, 92 (1850).
The engineers, however, have not succeeded in grassing all the slopes, and fallen
fossils may still be picked up at the base.
_ ¢ Bed 18 of Dr. Wright, who describes it correctly in Warden Cliff, but
appears to have mistaken its position in Headon sub (2b. p. 95).
Q.J.G.S8. No. 146. I
102 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
Marine series above the Neritina-bed,is some foxy-coloured sand-
rock, while lenticular layers of white sand are seen thinning out in
the grey clays, which also contain red-clay ironstone nodules, a dif-
ferent lithological condition from what occurs further north in the bay,
or to the south of Warden Point. Above comes the richest part of the
Venus-bed with abundant Cytherea incrassata ; these fossils not only
strew the tumbled clays, but with other fossils are commingled by the
waves with recent shells on the strand. Atthis point of the bay Ostrea
velata is very abundant above the part richest in Cytherea.
In the centre of the bay between Colwell and Bramble Chines |
this oyster is in extraordinary abundance; at one place it nearly
crowds out most of the other fossils, and forms a massive oyster-
bank about 21 ft. thick *, of which the lower 12 ft. is almost
made up of these shells. The ordinary character of the Venus-
bed is quite altered here, though its fossils occur mixed up with
the oysters; we may notice as especially abundant Murex seaden-
tatus, Pisania labiata, Natca labellata, Nerita aperta, Cerithium
variabile, Ostrea velata, Nucula headonensis, Cytherea merassata, &c.
On either side of this spot, near both How Ledge and Bramble Chine,
the excess of oysters has disappeared, and they are chiefly abundant in
a zone above the richest part of the Venus-bed, though they do occur
sparingly throughout. Cytherea merassata occurs through several
feet, but the richest part of the Venus-bed consists of about 9 inches
of bluish-green sand ; in this the shells are found in the best state
of preservation. Above the grey and greenish-grey sandy clays
richest in marine forms are some pale bluish-green clayey sands,
between Bramble and Linstone (or Lynchen) Chines ; in these, at
the level of about 5 feet from the base, is a band very rich in Ceri-
thium ventricosum, C. variabile, Melania muricata, Corbicula obovata,
with, occasionally, Verita ; this bed is seen just beyond the spring at
Linstone Chine, it is only a few feet below the base of the Upper
Headon. We wish to draw attention to the first-named fossil, as it
occurs also near the top of the marine beds at Headon Hill, 7. ¢. in
quite an analogous position.
Upper Headon of Colwell Bay.—The slate-coloured grey clay with
Potamomya ~ (ammediately succeeding the bluish-green sands) we
take as the base of the Upper Headon. A detail vertical section
is given (fig. 3), in order to show the lithological differences
existing between the series here and equivalent beds in Headon Hill.
We do not, however, think them greater than the differences already
noticed as occurring in the marine series in different parts of Col-
well Bay, while the resemblances are sufficiently great to allow of
their perfect correlation—not to mention their position between the
Osborne beds above (so identical with the Osborne beds of Headon
Hill) and the marine series below, which we have shown, on strati-
graphical grounds, is most certainly identical with the Middle Headon
of Headon Hill. The differences consist here in a greater develop-
ment of sand and a reduction of limestone: the sands at the base
* Bed 12 of Dr. Wright (zd. p. 92), who, however, much underrates its thickness.
t Base of bed no. 5 of Dr. Wright (2d. p. 91).
HEADON.
UPPER
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 103
Fig. 3.— Vertical Section A Upper Headon Beds in Colwell Bay.
(Scale, 8 feet to 1 inch.)
Paludina lenta, Pota-
Light-grey clays, with layers of shells. ; momya gregaria, 8c
Pale brownish-grey and light-brown clays in alternations.
ft. in
15 0
5 : _ 3. § Corbicula obovata, Cy-
0 6-9 Nodular band offerruginous sand-rock.) “7 Ty» Sete 2 x
Whitish sand above, yellow and ORE NYRI, I MAE
24 eee eee ears z lenta, Corbicula obovata,
Torn y ; Melanopsis fusi ormis.
Th al a " { Mi) | Buff-coloured TZimnea-limestone, with carbonaceous layer
li th ali | below.
16 > Pale greenish-grey clays.
SS Zone of Cerithium trizonatum.
———————=| Pale greenish clay.
ew == Ferruginous sand layer.
== Paler sandy clays.
Cyrena Wrightii, Corbicula obo-
io Stiff slate-coloured grey clay.4 vata, Melanopsis fusiformis,
= Paludina lenta.
5 6 Varying alternations of paler and darker grey clays.
= : Pale buff-coloured sands, with lignitic or carbonaceous bands.
15 0 2
rede ssene ts
re, ee 2 ee or | Greyer sands below. Potamomya,
a roonn
ee. aa: AO ee
otal’... 463 feet
Bo
104 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
are considerably thicker here than at Headon Hill; their character
is very variable even in different parts of Colwell Bay. The
Limnza-limestone has here a much reduced thickness, as mentioned
previously.
Among the other beds we may specially notice the horizon of
Cyrena Wrightw; it occurs in the nodular ferruginous sand-rock
with Corbicula obovata, also in the sand immediately above the
Limnza-limestone, and again in some of the clays below. Another
fossil that we have only observed at one horizon is the Cerithium
trizonatum (Morr.); it occurs in the pale greenish clays beneath the
limestone, occupying only a narrow band in these clays. Equally
characteristic is Serpula tenuis (Sow.), which occurs at the same
horizon both here and at Headon Hill, viz. in the Upper Potamomya-
clay just above the limestone.
The Paludina-clays at the top are identical with those of Headon
Hill at the top of the thick limestones. Measurement by tape here
gave 15 feet ; total of the Upper Headon near Cliff End 46} feet.
Osborne Beds of Cliff Hnd.—The red and greenish mottled marls
of the Osborne series follow. These beds show for afew yards only,
and then become hidden under the grass which the engineers have
grown on the artificial slopes below the battery. One of us well
remembers the numerous little faults (14 are enumerated by the
Survey, as cited above) which repeated the Limnza-limestone.
Beyond the battery the Osborne beds form the tumbled cliff; a
measurement is no longer to be made with profit. Mr. Bristow
gives 62 feet for the series here.
III. PanxontToLogicaAL EVIDENCE.
The question now arises, Does the distribution of fossils bear out
the separation of the Colwell-Bay and Headon-Hill marine beds
and their reference to different horizons ? and does it sanction the
notion of the Brockenhurst bed being equivalent to the Colwell-Bay
bed ?
Two lists of fossils are laid before us, viz. one which mixes up the
fossils from the Brockenhurst, Whitecliff Bay, and Colwell-Bay
localities, and the other which gives those from the marine beds of
Headon Hill and Hordwell Chiff; of the hundred forms (in round
numbers) which occur in the latter list, it 1s said (op. cit. p. 150)
‘less than one half occur at the other three places.”
We may urge at the commencement that it comes rather near to
begging the question to mix up Colwell-Bay with Brockenhurst-series
localities. We conceive one of the main points in dispute to be
whether the Colwell-Bay bed has any more affinities with the
Brockenhurst fauna than has the Headon-Hill bed; and to this sub-
ject we shall address ourselves after we have first compared the
fauna of the Colwell-Bay and Headon-Hill marine beds.
The first thing to be done is to separate the faunas of all the
localities which are to be compared together; this we have done in
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 105
the lists at the end of this communication. These have been drawn
up from an inspection of the Edwards collection of Tertiary fossils
in the British Museum ft, while we have added many occurrences
from our researches this summer, and we believe our list to be fairly
correct.
We do not admit that the Edwards collection is sufficient for a
full knowledge of the distribution of English Tertiary fossils: ¢.g. if
a certain shell does not exist in the Edwards collection from Colwell
Bay, it is no proof that it does not occur there, but simply that
Mr. Edwards had better specimens of it from Headon Hill, which
was considered, as, indeed, it is, an equivalent bed. The greater
part of the Edwards collection was made by the hands of one of the
authors; but we do not think it possible to establish from this col-
lection that Colwell Bay contains so many marine forms which do
not occur in Headon Hill, and therefore that the marine beds at these
localities are not on the same horizon.
The following reasons induce us to say this:—It was the habit of
the local collectors to exploit the Colwell-Bay bed far more than the
Headon-Hill locality, because it was more accessible and showed
a larger extent exposed ; the fossils were better preserved, and in
every respect it was easier to collect from. Again, some species
which one of us supplied to Mr. Edwards from Headon Hill were
not incorporated in this collection, probably owing to his having
better ones from Colwell Bay; and doubtless they were exchanged
with foreign correspondents or given away. These two con-
siderations would serve to account for his Colwell-Bay collection
being richer than his Headon-Hill one. Corroborative of this is
the fact that in a few days’. search this summer we have found
several species in the marine bed at Headon Hill which do not exist
in the Edwards collection from that locality.
Moreover we hold that the best test as to the contemporaneity
of these beds is not to be obtained from the rarer forms, which may
be evidenced only by a single example, but from a comparison of the
commoner, which we should consider the more characteristic forms.
Accordingly we add a list of the species obtained by us this summer
from the Middle Headon of both localities: H indicates Headon
Hill; C the equivalent bed at Colwell Bay.
List of all the Shells obtained on the ground by the authors for the
purposes of this paper (Aug. 1880).
(Those with an asterisk pass up from Barton beds.)
*Lamna contortidens (4g.) ... C,H. | *Borsonia sulcata(fouw.)......... C.
Marginella vittata (Hdw.)...... H. | *Rimellarimosa (Sol.) ......:.. OVE
*Voluta spinosa (Lam.) ......... C, H. Murex sexdentatus (Sow.)...... Opal
or otoma headonensis (Hdw.).C, H. BPs Seen eee Cees on awetces lek
denticula (Bast.), var. Pisania labiata (Sow.) ......... CO, H.
odonbellat(Hd.) os. 5.00.42 C,H. | *Cominella flexuosa (Hd. MS.) O, H.
t We are greatly indebted to the Keeper of the Geological Department, Dr.
H. Woodward, F.R.S., for his courtesy in allowing us access to the collection,
even during the laborious process of packing up and moving the national col-
lection to the new buildin g at South Kensington.
106
H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
List of Shells (contenued).
*Ancillaria buccinoides (Lam.) C, H. Planorbis euomphalus (Sow.) C, H.
*Natica Studeri (Bronm)......... C, H. obtusus (Sow.) .........00. C,H.
labellata (Lam.) ......... @), dal Paludina lenta (Sow.) ........- C,H.
Cancellaria muricata (Wood) C, H. Ostrea velata (Wood) ......... C, H.
elongata (Nys?)..........+ C,H. | *Mytilus affinis (Sow.) ......... C, H.
Odostomia gracilis (Hd. MS.) C. *Trigonccelia deltoidea (Lam.), OC, H.
Scalaria tessellata (Hd. MS.)... C. Leda propinqua (Wood) ...... C, H.
*Cerithium yariabile (Desh.) ... C, H. Nucula headonensis (forbes) C, H.
we pseudocinctum (d’ Ord.) CO, H. nudata (Wood)... <2... C, H.
duplex GSow:) ae. sees H. Lucina (Strigilla) colvellensis
ventricosum (Sow.) ...... OC, H. (Ed « MS.) 05 occ eeceeeeeee C,H.
varians (Hd. MS.) ...... C,H. | Cytherea suborbicularis
—— (Vicarya) concayum (Od MIS. Vins Sine eee C,H.
(SOU) ca tn owilnvecturboaecmees Cons incrassata (Sow.) ........- C, H.
Melania fasciata (Sow.)......... C, H. Tellina headonensis (Hd. MS.) OC, H.
muricata (Sow.) ......... C,H. | [*]Psammobia compressa (Sow.),
Hydrobia bulimoides (Hd. MS.) C, H. var. estuarina (Hd. MS.)... C, H.
Melanopsis subfusiformis rudis: (Lane) eee eee C, H.
(GUGIS anecion waoaatocadoasec SG, Ee Mactra fastigiata (Hd. MS.).,. C,H.
fusiformis (Sow.) ......... C,H. | *Mya angustata (Sow.)=pro-
Acton dactylinus (Ed. MS.) . C. ducta (2d MiS)) ieee eee C,H.
Nematura parvula (Desh.) C,H. | *Corbula cuspidata (Sow.) ...... C,H.
Nerita aperta (Sow.) .........5 55) (O4dab Corbicula obovata (Sow.) ...... CoE
zonula) CHW 00d) <...2-2ke-- C,H. Cyrena cycladiformis (Desh.). C, H.
Neritina concava (Sow.) ...... C,H. | *Balanus unguiformis (Sow.). C, H.
Bulla estuarina (Hd. MS.) ... CO, H. Callianassa Baylu (Woodw.). C,H.
Limneea longiscata (Sow.)...... C, H.
Faunas of Middle Headon from Colwell Bay and Headon Hill
compared.
The above list contains only the commoner forms, such as may be
found in a few days’ search. Out of a total of 58 species it will be
observed that all but 7 were found by us in both localities *, and all
but three are known to be common, or, again, a proportion of 94 per
cent. of commoner Colwell-Bay forms occur.at Headon Hill. Surely
from this we may presume a very close .affinity if not idence of
these beds. It is stated (op. cit. p. 150) that less than one half of
the Headon-Hill and Hordwell species occur at Colwell Bay—a
result, it seems to us, only obtained by mixing up fossils from
Brockenhurst and Whitecliff Bay in the same list with the Colwell
forms. We shall show below that the fossils cited from these two
latter localities belong to a lower zone.
Next as to the statement that at Colwell Bay “ the strata are of
purely marine origin” while “ the so-called Middle Marine beds of
Headon Hill and Hordwell Cliff are of totally different character ”
* Some of these do not exist from both localities in the Edwards collection,
val have not found their way into the Headon-Hill.and Hordwell list in the
paper referred to, though previously cited by Dr. Wr ight: from Hordwell
ib. p. 124).
~ Comparing the whole known fauna from the Middle laid of Colwell Bay
and Headon Hill, we obtain the following result, viz..74-per cent. of the
Colwell-Bay marine forms have been found at Headon Hill. ‘This is counting
as separate species many names in the Edwards collection which are founded on
imperfect and single specimens. As we have said, we think a surer guide in
comparing faunas is to take only the characteristic and less rare species.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT, 107
&e. (l.¢. p. 148). Of the brackish-water genera which are supposed
to be found in Headon Hill only, we may remark that we found
Cerithium, Cyrena, Hydrobia, Liamnea, Paludina, Planorbis, Melania,
and Melanopsis fully as plentiful m the marine series of Colwell
Bay as at Headon Hill; e.g. in a quarter of an hour we turned out
half a dozen specimens of Limnea longiscata* from the richest
nine inches of the Venus-bed, the best zone for Voluta, Cancellaria,
Murex, Cytherea, &c. It has always been the opinion of one of us,
who has worked these beds for so long, that these freshwater forms
were either drifted down by flood-waters or were dead shells washed
out of lacustrine or brackish deposits. They cannot have lived in the
waters depositing the marine bed at Headon Hill any more than at
Colwell Bay.
Another argument brought forward in opposition to the views of
the Geological Survey is, that certain species of Cerithiwm are
confined to Headon Hill and do not occur in Colwell Bay; and by
this means have been “ detected the serious errors which have crept
into our classification and correlation of the strata we are now con-
sidering” (op. cit. p. 149). Cerrthiwm ventricosum and C. concavum
are said to be entirely confined to the Headon Hill and Hordwell
localities. We cannot agree with the statement as to the distri-
bution of C. ventricosuwm in the Headon-Hill beds and its “* prodigious
abundance.” It is there, as far as we have observed, found only in
one bed; moreover, it is equally abundant in a bed in a precisely
similar position at Colwell Bay, viz. at the top of the Middle Headon.
Its analogous position in these two localities we consider as fossil
evidence confirmatory of the stratigraphical.
Nor do our observations confirm the statement of “ prodigious
abundance ” of C.(Vicarya) concavum at Hordwell Cliffin the Middle
Headon. One of the authors who worked that bed when a special
excavation was made for the purpose‘, considers that V. concava
was extremely rare in the Hordwell bed; but, as is well known, it
occurs abundantly in the Upper Bagshot sands further west at Long
Mead End.
As to the supposed absence of V. concava from Colwell Bay, we
remark that we had not been many minutes at work on the richest
portion of the Venus-bed before we found a specimen, subsequently
followed by a dozen more. It can scarcely be maintained, therefore,
that the Colwell-Bay bed does not belong to the C.-concavwm zone.»
This species is here, however, not so common as at Headon Hill +.
* Also noticed by Mr. Bristow, F.R.S. (Mem. 10*, p. 61), as well as by previous
writers.
t The Middle marine or Middle Headon bed at Rook Cliff, Hordwell, has not
been exposed for the last twenty-eight years ; it is covered up by a great thick-
ness of gravel, and its precise position is known but to few geologists. It was
quite a thin bed, but rich in fossils, especially minute forms. Fossils in
existing collections were all obtained about a quarter of a century ago.
{ This species exists, however, in the Edwards collection, labelled as from
Colwell Bay. The absence of a shell in the Edwards collection from Colwell
Bay is no proof that it did not occur there; the local dealers might not have
thought of picking up V’. concava at Colwell Bay. For this species they went
to Headon Hill, where it was more abundantly found and in better preserva-
108 H, KEEPING AND E. B. TAWNEY ON THE BEDS AT
Summary.—There is but one marine bed here, namely that in
the Middle Headon ; for the Colwell-Bay bed can be traced strati-
graphically into the Headon-Hill Venus-bed, and the paleontological
evidence 1s in harmony with the stratigraphical. The place of the
Brockenhurst bed is at a lower horizon in the Middle Headon ; but
it does not appear anywhere in the west end of the island.
TV. Watreciirr Bay anp New Forest.
Middle Headon of Whitechff Bay—We next have to raise a
more serious objection to the way in which the Whitecliff Bay
section has been interpreted. In mixing up all the beds in the
marine series there together and calling them Brockenhurst series,
it seems to us that the question has been obscured, if not begged.
The statement is that the 100 feet of marine beds at Whiteclifi Bay
are the equivalents of the 25-feet of marine beds at Colwell Bay and
of the beds in the New Forest with the Brockenhurst fauna (op. cit.
148). Hence the Colwell-Bay bed is placed in the Brockenhurst
series, which is said to occupy a higher horizon than the Headon-
Hill and Hordwell marine bed; and this view is indicated by dotted
lines in the vertical sections on p. 170. Since the 100 feet of
marine beds are classed together and called *‘ Brockenhurst Series,”
we suppose that the Brockenhurst fauna is imagined to occur
throughout them. Asa matter of fact, that fauna is confined to
one zone, and that the very base of the series.
Though we have worked over this part of the section bed by bed,
we need not here give all the details, but will refer to the description
of it on the Survey Vertical Section on Sheet 25. This series is
there justly referred to the Middle Headon, since it lies between the
freshwater Lower and Upper Headon, its total thickness read off
by scale being 90 feet. At the top are clayey sands and yellow
sands about 19 feet; then the “ Venus-bed” clays &c., 15 feet;
next, below, are compact sands with nodules about 42 feet, said to
contain Sanguinolaria Hollowaysii*; then come 14 feet of brown
clays, the base ‘‘ greenish and brownish clay, very fossiliferous.”
Now there is no doubt at all about the bed above and the Venus-
bed here being any thing but the Colwell-Bay and Headon-Hill
marine bed—its position and its fossils prove that; the characteristic
Brockenhurst fossils are absent from it, and it is therefore certain
that it differs entirely from the Beeeonheret beds.
The Sanguinolaria-sand differs lithogically from the lower part
of the marine series, both at Colwell Bay and at Headon Hill. Such
few fossils as we observed in it are distinctive, not of the Venus-
tion. Moreover these collectors sought to obtain as many forms as possible,
but were not concerned in finding the same species in both localities; and if
they found only a few stray examples at one locality of a species of which they
had a great number from the other, they were liable not to put a separate label
for the odd few, but to mix them up with the larger parcel.
* A wrong determination; the shell is Psammobia compressa, var. estuarina,
Kd. MS. It occurs in the natural position of life, 7. ¢. across the bedding.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 109
bed, but of Brockenhurst beds; but though we have not sufficiently
worked out this fauna, we may say that we are satisfied that they
belong to a lower zone than any of the marine beds at Colwell Bay
or Headon Hill, the Middle Headon being more fully developed at
Whitecliff Bay than elsewhere.
Brockenhurst Zone at Whatecliff Bay.—The succeeding 14 feet
are the equivalents of the Brockenhurst beds; the lowest two feet
we shall call the Brockenhurst zone ; the remainder of the thickness is
not nearly so rich in species, and their grouping, as well as the litho-
logical character, is more lke that of the Roydon beds.
At the time the Survey section was made, the interesting bed at
Brockenhurst had not been discovered nor its fauna described;
hence such Brockenhurst fossils as were found in this zone here
were not rightly determined (thus in the Survey section we must
read Cardita deltoidea, Sow., for C. acuticosta), or specific names
were withheld from them. Subsequent observers* have recognized
the Brockenhurst fauna in this lowest bed. As we have obtained
more fossils from it than previous observers, we have embodied our
results in a separate column in the lists at the end of this essay ;
that column contains nothing except what we have collected with
our own hands this summer from the lowest two feet +, lying on an
eroded surface of the freshwater Lower Headon. Comparison of this
list with the fauna from Brockenhurst itself will convince most, we
think, of the perfect equivalence of the zone in the island and in
the forest, while its position at Whitecliff Bay shows that it is at
the base of the Middle Headon.
Brockenhurst Zone in the New Forest.—The greater part of the
fossils from Brockenhurst were collected by the hands of one of
the authors, and thence were dispersed into various public and
private collections. They were obtained during the doubling of the
line and widening of the cutting at Whitley Ridge, near Brocken-
hurst t, about twenty-three years ago. During this work he had
- the advantage of seeing more of the beds than any other geologist.
He found the rich Brockenhurst zone (which varied from a few
inches to nearly a foot) lying immediately upon the freshwater Lower
Headon ; while about half a mile up the line, near the bridge by
Lady-Cross Lodge, the Middle Headon Venus-bed was seen, followed
by the freshwater Upper Headon beds above, the beds having a very
gentle dip up the line oreasterly§. It is evident that the succession
* Videlicet Von Konen, Quart. Journ. Geol. Soc. vol. xx. p. 98; Rev. O. Fisher,
Quart. Journ. Geol. Soe. vol. xviii. p. 67, footnote; Mr. T. Codrington, Quart.
Journ. Geol. Soc. vol. xxiv. p. 519; Dr. Duncan, Pal. Soc., ‘ Fossil Corals,’ i.
p- 40 (1865).
t In the Edwards collection the label “ Whitecliff Bay” includes many
Venus-bed forms, indeed Lower and Upper Headon, or it may be any thing
from the London Clay to the Bembridge Marls; there is therefore good reason
for not allowing this collection to stand as evidence of what is found in the
Brockenhurst zone at Whitecliff Bay.
{ The railway-cutting at Brockenhurst (op. cit. p. 152) refers to the same
spot as Whitley Ridge.
§ We visited the New-Forest localities together this summer, and found the
Whitley-Ridge cutting entirely grassed over (the rich zone was below the level
110 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
here is, in ascending order, freshwater Lower Headon, Brockenhurst
zone, Venus-bed, then freshwater Upper Headon, which agrees
with the succession in Whitecliff Bay. Yet in the New-Forest
section (op. cit. p. 170) we find the Brockenhurst bed placed above the
marine band or Middle Headon of Totland Bay—in other words,
the natural succession is inverted.
Again, in Headon Hill as we have seen, an imaginary Brocken-
hurst bed (of which the Colwell-Bay Middle Headon is stated to be
the equivalent) is placed above the Upper Headon, in ground which
is really occupied by the Osborne beds. If the Brockenhurst bed is
at a higher horizon than the Middle Headon of Headon Hill, then
where is the marine Middle Headon at Whitecliff Bay ?
We can scarcely adopt a theory which makes the Colwell-Bay bed
occupy a higher horizon than that of Headon Hill, because it is
supposed to contain more Brockenhurst fossils, when the latter
fauna is found below the zone with (Colwell-Bay or) marine Headon
fossils both at Whitecliff Bay and near Brockenhurst. When once
the position of the Brockenhurst fauna is recognized (and it has
been correctly described by previous observers), the inconsistency of
the theory is apparent,
Affinities of the Brockenhurst Fauna.—Seeing that the Brockenhurst
fauna, if different in age from the Marine Headon, is older, instead
of being younger, it would be rather anomalous to find that “ while
nearly one third of the Hordwell and Headon-Hill marine shells are
Barton forms, not more than one fifth of those occurring at Brocken-
hurst, Colwell Bay, and Whitecliff are found at Barton.” We have
already mentioned one feature in the lists on which this statement
is based by which the question is almost begged. We must next
allude to what seem to us clerical errors, in order to justify the
very different statistics which we have obtained by inspection of
the Edwards collection, supplemented by our own researches.
In the Headon-Hill list we observe nine species* that are said
to pass down into Barton beds, while in the Brockenhurst list this
range is denied to them; and besides these nine, the range into
Barton, as proved by the Edwards collection, is omitted in the Brock-
enhurst list in the case of twenty-two other species. Discrepancies
of this sort must seriously detract from the value of any statistics
based on such lists.
of the rails, and will never be seen again here); the upper beds were yellowish
clayey sands, poor in fossils. Sufficient characteristic Brockenhurst fossils may
still be seen, however, on the old spoil-banks of the date of the making of the
original single line, about forty-two years ago. By Lady-Cross Bridge the
cutting is also grassed over ; but evidence can still be found of the Venus-bed
in the side drains and of the Upper Headon in the slopes above it.
* These species are—Borsonia sulcata, Nematura parvula, Mytilus strigil-
latus, Cardium obliquum, Trigonocelia deltoidea, LIncina obesa, L. concava,
Panopea subeffusa, and Scintilla angusta. On the other hand, an error on the
opposite side, omitting the range into Barton beds in the case of Marginella
simplex and Corbula cuspidata, goes only one quarter of the way towards
redressing the balance.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. pa
So far from the Brockenhurst zone having fewer forms common
to the Barton than the Headon-Hill marine bed, we consider that
it has rather more, as its position at the base of the Middle Headon
at Whitecliff Bay would lead us to expect. Thus, if we take the
whole Brockenhurst fauna (including the 15 corals which are mostly
special to the zone), we obtain a total of 151 species, of which from
74 to 81 pass up from Barton, or a proportion of about one half.
Summing up the Headon-Hill forms in the same way—out of a
total of 79 species, 23 pass up from Barton beds, or a proportion of
29 per cent. But, instead of including the rarer forms, if we take
only the more characteristic and abundant species of the Brocken-
hurst zone, it would be perhaps a preferable course.
The following list is a catalogue of the fossils in the Woodwardian
Museum from the Brockenhurst zone, obtained by one of us many
years ago at Whitley-Ridge railway-cutting, New Forest; and it
may be taken to include the chief characteristic fossils of the zone.
We have found all, except two, in the 2-feet bed at Whitecliff Bay
this summer.
xInfundibulum trochiforme = obli-
quum (Sow.).
*Hippocrenes (Rostellaria) ampla.
*Rimella rimosa.
Murex hantoniensis (Hd. MS.).
xTyphis pungens,
*Strepsidura armata.
Cancellaria muricata.
Pisania (Fusus) labiata.
*Clavella (Fusus) longeeva.
Leiostoma ovatum,
xCassis ambigua.
Ancillaria buccinoides.
Pleurotoma transversaria.
cymezea.
headonensis.
¥ denticula.
% pyrgota.
oo decora (Beyr.) = maga
é).
* spinosa.
suturalis.
geminata.
xActezon simulatus.
Marginella estuarina.
xNatica hantoniensis.
* Studeri.
x— , var. grossiuscula (Hd.
MS.).
x—— labellata.
Chenopus Margerini, var. speci-
osus,
Phorus eretifer (Ed. MS.).
Ostrea ventilabrum = prona (S.
Wood).
xAnomia tenuistriata.
Pecten bellicostatus,
Modiola Nysti.
xAvicula media.
xLucina bartonensis (Ed. MS.).
x Cardium porulosum.
Protocardium hantoniense (Hd.
MS.).
Cardita deltoidea.
xCytherea incrassata.
suborbicularis (Hd. WS.).
Solandri.
Cyprina Nysti.
*
[x]Crassatella Sowerbyi, var. hanto-
niensis (Hd. MS.).
xCorbula ficus.
x cuspidata.
[x]Psammobia compressa, var. arcu-
ata (Hd. MS.).
Panopeea sulculosa (Hd. MS.).
Madrepora anglica.
Dendrophyllha.
Lobopsammia cariosa.
Balanophyllia granulata.
Solenastrza cellulosa.
Of this shorter list a proportion of about 50 per cent. pass up
from Barton or Bracklesham beds; so that, taking the whole fauna
or the more characteristic members of it only, in either case nearly
one half pass up from Barton beds—a very different thing from one
12 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
fifth, which was the proportion given in the paper referred to (op.
cit. p. 150). If we compare with this the ratio of Barton forms in
the list of commoner Headon-Hill given above (supra, p. 105), we find
that 30 per cent. pass up from Barton beds (while in the complete list
of the Headon-Hill fauna the porportion is also about 29 per cent.).
Moreover, if we first eliminate the forms that occur also at Brocken-
hurst, so as to obtain what we may consider as specially Headon
species, the proportion becomes even lower. On all hands the
paleeontological evidence seems perfectly in accord with the strati-
eraphical.
Relation of Colwell Marine to Brockenhurst Fauna.—In order to
see whether the Colwell bed is more nearly related to the Brocken-
hurst than is the Headon-Hill bed, we will first take the proportion
of Barton forms in it for comparison with similar treatment of the
Headon-Hill catalogue. Examination of the list gives us a pro-
portion of 29 per cent. of Barton forms in the Colwell-Bay bed; we
saw above that, in the Brockenhurst bed, the ratio was about 50 per
cent. and in the Headon marine bed 29 percent. An inspection of
the list of more characteristic Colwell and Headon marine fossils
(supra, p. 105) showed that these faunas are practically identical
Now we see that their proportion of Barton forms is nearly equal,
and far lower than in the Brockenhurst bed.
To complete the proof from fossils, if any such is needed, we may
inquire whether there are more Brockenhurst forms peculiar to
Colwell Bay than to Headon Hill. Examination of the lists
shows that only the following Brockenhurst species occur at
Colwell Bay and not at Headon Hill, viz. Scalaria tessellata
and Tellina affinis, the latter passing up from Barton beds;
while those occurring at Headon Hill and not at Colwell Bay are
Marginella estuarina and Cardita paucicostata—two only in each
case, which amounts to perfect equality. If, on the other hand, we
count those common to the Colwell and Headon marine beds, ail not
occurring at Brockenhurst, we find twenty-six species in this
category. We are at a loss to understand how any one could
imagine that the Brockenhurst fauna is identical with that of the
Colwell-Bay bed and newer than that of Headon Hill.
That the Colwell-Bay bed is stratigraphically identical with the
Headon Middle Marine we hope that we have sufficiently proved ;
and the fact is confirmed by fossil evidence. The same twofold
proof has been brought forward to demonstrate that the Brocken-
hurst bed, where present, lies at the base of the marine Headon
beds and immediately above the Lower Headon. This bed is
absent at Colwell Bay and Headon Hill, but is seen at Whitecliff
Bay, Brockenhurst, and Lyndhurst.
Since the Middle Headon includes every thing between the fresh-
water Upper and Lower Headon, it must be allowed to include fhe
Brockenhurst beds, though that special fauna was not known when
names were given to these groups of strata. It would cause the
ereatest inconvenience to abandon the term Middle Headon, as it
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. Lis
would entail the abandonment of the names Upper and Lower also.
There is therefore no room for the term ‘“ Brockenhurst Series” in
the sense proposed in the paper referred to (op. ct. p. 168)—a
classification which would be in conflict with the best authorities,
and founded, as we have endeavoured to show, on a defective appre-
ciation of the beds. We may urge that no new facts have been
discovered concerning the succession of the strata to make any
correctionary classification or nomenclature in the main groups of
the Upper Eocene at all necessary or desirable, and we should prefer
to retain the local groupings which have been so long familiar to
geologists. We may denote as the “ Brockenhurst Beds ” the lower
part of the Middle Headon with the rich Brockenhurst fauna. It
is not always developed; the absence of admixture of fresh water
was evidently the necessary condition of its abundance of marine
mollusca and of the existence of its corals.
It may perhaps be subdivided into the “‘ Brockenhurst zone” and
the ‘‘Roydon zone”*. The correlation of this fauna was justly made
* We found the Roydon brick-yard pit in a good state for examination this
summer, and obtained from it twenty-eight species. They all came from the
sandy clays with bands of iron-ore septaria; the lowest beds were below the
level of the standing water. ‘The section is as follows :-—
Gravel, Post-Tertiary.
2-3 feet. Bluish to yellow-grey clay.
( Murex -sexdentatus, Cardita ob-
| longa var. transversa, Pisania
Gr hies { ‘“Shell-bed ;” clay very full of 4 labiata, Trigonocelia deltoidea,
5 shells. | Ostrea velata, Cytherea incras-
| sata, Cyrena obovata var..sub-
\
regularis (Ed. MS.).
Voluta geminata, Voluta spinosa,
Strepsidura armata, Pleuro-
( Grey clay.
| toma transversaria, Pleuro-
| Two nodule-bands of iron-ore
4 feet. | septaria separated ° Sune: ae
7 feet 4 1 pare by grey toma hantoniensis, Natica
} sandy clay. ; 1 , .
eee 9 epiglottina, Bulla Lamarckit,
| Stiff bluish clay for the lower 2 . Sete
leet Protocardium hantoniense,
: Cytherea suborbicularis, Psam-
mobia estuarina, Corbula
pisum, &e.
7 feet. Greenish-grey clayey sands.
—
Reposing on Lower Headon fresh-
water clays.
The shelly bed, we consider, represents part of the Venus-bed or Headon-
Hill marine zone, since it contains the characteristic oyster and Murex sexden-
tatus, &e.
The clays and clayey sands below, of which we examined 74 feet, while,
according to the statement of the men employed, the remaining sandy beds
below are another 7 feet, we propose provisionally to term the “ Roydon zone.”
Tt is characterized paleontologically by the abundance of Voluta geminata,
differing from the “ Brockenhurst zone” by the absence or great rarity of Voluta
suturalis, Pleurotoma cymea, and Cytherea Solandrz, for the latter shells are
114 H. KEEPING AND E, B. TAWNEY ON THE BEDS AT
by Von Konen in 1864, and by Dr. Duncan for the corals in 1866,
whose work is not in any way affected by any thing in the present
essay. We have merely striven to prevent the beds in the Isle of
Wight and the New Forest being thrown again into confusion, and
the accurate work of EK. Forbes and the Geological Survey being
rejected on such insufficient grounds as have ‘been recently put
forward.
abundant in that rich zone, a few inches thick, in the Whitley-Ridge railway-
cuttin
At the time of obtaining the Roydon fossils in the Edwards collection, one
of the authors sank a pit to the base of these beds, and they were found lying
immediately on the freshwater Lower Headon clays, the Brockenhurst zone
being absent; the latter has apparently thinned out here, as the Roydon zone
itself thins out a little further west.
Of the White-Cliff Bay beds we are disposed to place i in the Roydon zone all
those between the ‘‘ Venus-bed ” clays of the Geological Survey Vertical Section
and the lowest two feet of sandy clays lying immediately on the eroded surface
of the freshwater Lower Headon, which said bed we have described above as the
“ Brockenhurst zone.” The Roydon zone will thus include the 42 feet of yellow
and green sands with ironstone-nodules, of which the chief fossil is Psammobia
estuarina (=Sanguinolaria Hollowayst of the Geological Survey Section), also
the remaining 12 feet of beds described in the legend as “brown clay,” but
which in their unweathered condition are slate-colour to greenish grey.
We had unfortunately not sufficient opportunity to work out the fauna com-
pletely; but such fossils as we found induce us to parallel these beds with those
of the Roydon brick-pit. The lithological character of these lower beds, as seen
below low-water mark at equinoctial tide, is singularly like the clayey sands of
the Roydon brick-yard, while their chief fossils are the Psammobia, lying in the
natural position of life, and Cardita deltotdea. At some future time we hope
to work out the fauna more completely.
At Cutwalk hill, Lyndhurst, both the Brockenhurst and Roydon zones occur.
In the pits which one of the authors sank in obtaining fossils for Mr. Edwards
and others from this locality, the Brockenhurst zone was found lying, as usual,
immediately on the freshwater clays of the Lower Headon.
Hence we may divide the Middle Headon into three zones, distinguishable
easily by fossils (though, of course, many species are common to all three), viz.
the Brockenhurst, the Roydon, and the Venus-bed or Headon-Hill zone. The
percentage of Barton forms diminishes as we ascend in the series.
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. aly
Fossils of the Middle Headon series, including the Brockenhurst
beds *.
Mippie Heapon.
UprEr
Brockenhurst |Baagsuor.
beds.
Be :
. os} ~
See es Loe,
SCRA rk se iene lees
® qd]jc sl | SS 5 Si ly.
= S) a 5 2ijf}] 4 lines
mS | = | SO = S 3) ceo
Ei slaielel/e12| #3
ee] fe tS Ge) ee tase | ea | 9s
xLamna contortidens (Ag.) ......... ee mae eg « |K.T. K.T.
Marginella simplex (Hdw.)......... shew lien ec Mi ctestet torte 50 *
estuarina (LdW:) 2 ssccss- dae | pe * *
—— Vittata (Hdw.) .........sceeseees con ||:
Voluta geminata (Sow.) ............ noo ees x |K.T.) x
— var.tereticosta(Hd.MS.)| ... |... | ... | * | *
% decors @Bey7,.)—maga (Hd.).| ... ||... |... |... (KT) x | x
suturalis (Mysz) = contabu-
[EUG (JEG) ih ORO ie Aa ee eee A iy Oem eae Glico at Gee Rn 2 lia
* SIMON CHAI)! Vesetaesacko ces x |K.T.) « | x |K.T.) «x | *
Mitra gracilenta (Hd. MS.)......... Sisteeall meted esate | ie
apmcenmiatan (HO neVLS. yess ectesclcoae || veces |v eines. vooes (Woelyl) eae |) 96
— polygyra (Hd. MS.) ......... Woe hrceiseahlpravo sis Wacetece litsione [itevictant| thee
[¥ |Conorbis dormitor(So/.), var. semi-
TUTOR CLUGAVE Vcasescce tase odasecsases ser ea semlinatisedl mend lieteate ta 9a! (UE
[x] procerus (Beyr.)=alatus, var.
Ienatllissey CHA ac. ce ces sede ecumese x |K.T.) x | x
Pleurotoma transversaria (Lam.) x |K.T.| x | x
Gyameear(HG.)) cli ecbecc noses ees Soe eo Ren pean eae ome ea De *
— var. nana (Hd.)......... Gon ates aay re
* YGC OA CHG.) ccs vepecsceset ec Shou epee toes es x
[ayes Dio kes (27000 Meee ee eee Bel ee Ae vse ate %
Pa NVOOUU CHA.) 20. ccececsesoseee Paes le oe
headonensis (Hdw.)............ x | « | « |K.T. i le as
* denticula; (Base.) 0.20.2. <s06: aes il ace Watereteel [iar
x— var. odontella (Hd.) .... x | « | * |K.TK.T.) x
—— leviuscula (EHd.) ...........-... ee alia w ales. Kane el) Serio peer [Ae
subdenticulata (Goldf.) =
hantoniensis (Hd.) ..........0.06: Bek Mal ncsatele| aceite | oes RGAE SSO Rae
* Borsonia sulcata (Mov.).........08. Ea ee cae eee 2a peer el 8
IOMMEP EER eitoncesen avd eriavioicieoa ve Cai leg, cabilitaeet tia ceht | ead Des
Chenopus Margerini(deKon.), var.
speciosa (Schlot.) ...........0e0.e0. Peeters i sacsc fh amie a | acer oe i ee
¥Rimella rimosa (Sol.) ............... San iB 36. =| 96S Ile ses KG aicseda aire
xHippocrenes (Rostellaria) ampla
DIGGS.) ), SACS CBAC BREA ee aan een ee Sse eee eh | eter | retoet VGA tea (3) lise
Carried forward ...... Bs Dey yy ep Ue’ IP Alte) 1
t Those marked with an asterisk pass up from Barton or Bracklesham
beds. The asterisk enclosed in brackets signifies that the type species exists in
Barton beds, but not the special variety. The initials K.T. denote that the
_ citation is the result of our own researches instead of being founded on the
Edwards collection.
116 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
Fossils of Middle Headon series, Jc. (continued).
Mippie Heapon.
Upper
Brockenhurst |Bacsuor.
beds.
= A x
P| Sis | 8 | 3 |e eee
sore as ss | “eS 3S an
Se ls | Sy a | Seems
ee popes |e te |
Brought forward je. sace re AND | SO oa aes 1
Murex hantoniensis (Hd. J7S.) 2.2)... |... | ..2 |) ce. (IK) See ee
sexdentatus (Sow.) ............ x | * | x
—— , var. cinctus (Hd.)...... Baca sea a liane
= MM (YSO/5) sestaccocosdtocads ck lela pili slau thy cme 9 Ges ee
*x—— obtusus (Desh.) ...........005- PP reel elton | age.|| 3
S)Db. MenoSdccbooqoocanonseos Sag Gelb
xTyphis pungens (Sol.) ............- wae if pete Te Bec] SRN ROS ea ie
Cantharus subcostatus (d.) ...... sae jegaaiel | Meee TN Meetsiona ected RRS
Fasciolaria crebrilinea (Hd. MS.)| ... | *
Pisania (Fusus) labiata (Sow.) ...| ... | * | * | * |K.T) « | x
-——, var. concinna ...........- Se ese
acuticosta (Hd@.) ............--- ae x
Phos scalaroides (Lam.) .....-...0+ x
*Clavella (Fusus) longeeva (Sol.)...) ... | --- | .. | * |K.T) x | x
Chrysodomus (Fusus) Sandber-
BENIN CL C0/774) gel eeacey eee a cre ets wae [cage ae AN Dec G [Pee eae eee
Leiostoma ovatum (Beyr.) ........- wes vesicle «/fteine a)! ceanall eee een Mi
xStrepsidura (Buccinum) armata
(CSIZTOD TENA Rkecr ne Bee EP A Len Sen wee |) bey | KCTS ia ae
semicostata (Hd. MS.) ...... *
xCominella (Buccinum) deserta
(ISOLDE tee eeneru oan ee von af vse ||) ateov'l|lleciesel| ACTS Pe ioe
flexuosa (Hd. MS.) .......4...: oie (KT |e 21) 20 a ie
ventricosa (Hd. MS_)......... MOR ore a ee
xAncillaria buccinoides (Lam.). ...) * |K.T.) *« | * |K.T) x | x
xCassis ambigua (Sol.) ............4.. wots [iedeisie vl toi fh pe | ERE Sa
*Natica hantoniensis (Sow.) ....... ase cose: | Senin. |. serie yt CGEIE ieee
% Obowatan (Sows) eaceeeenee eee uate md ata
conulus (Bo. MES iho ease. wee [icesecla'eo es [yee eee ieee Moe
Tea eaten wee Nes 96410. AE wal gael Ea a NG *
* yar. grossiuscula
(Ed. MS.) wie) Sia pee O eae Renee soe |. 9 | RAUS 20077|o2 Sn ee x
% epiglottina (Lam.) .........--- Dell Geers \useoy| Kaede
labellata (Lam)... ese S| eK ees aie
; var, dubia) Cid SES 9) seal) eee [leet me lceate | iratrell tater *
Cancellaria muricata (8. Wood)
Sloymexoes GIL WIS) Soosonncosee KOT.) | 30 KEM rn ae
elongata (Nyst) .....<......00. x [e56. | .3e L | ceo] Ree
* EMU (ISOUS)s<css ns seel eee BME Aare, /a|ttere [tee of eS
roydonensis (Hd. MS.) ...... SAS) Il ocean One esc
xPyramidella (Turbonilla) obscura
(LITE ULSI ONS ese ea nrnpmris ann eal ieee tessa oe
Turbonilla plicatella (Hd. ae seettllieee cine 1 toe
semilzevis (Hd. MS.) ......... cca etal eee Slane
plicatilis (Hd. MS.)............ noo || ooo || #8
Carried forward ...... 11 | 20 | 22 | 81 | 31 | 25 | 39] 8
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. ley
Fossils of Middle Headon series, dc. (continued).
MippiE Heapon.
aa ae |. UPPER
| Brockenhurst |Bacsuor.
beds.
a :
a |S fe le
Ss a)
See ale | alae &
slzlfi/sl/2l\2/2| es
Sao lov) Seley Ea ee ae
SiS Ole |e lala] A.
Brought forward ............ 20 22) Sloe 25: 839 3
*xTurbonilla obliquecostata(Hd.MS.)) ... | x
Guia (2d. MS.). 0.0 .sccscess S|. 296 |
sorella (did. MS.) ............ See
Odostomia loxodonta (Hd. MS.)...) ...) * | *
subumbilicata (Hd. MS.) ...) ... | * | x
geminata (Ed. MS.) ......... gee) | een |t 3
—— multispirata (Hd. MS.) ...... Sage |) 36
gracilis (Ed. MS.) ............ ser eed
x*—— hordeola (Zam.) ...........+08- |
—— , var. angusta (Hd. MS.)| ... | ... |... | *
Hulima gracillima (Hd. MS.)...... eel Cec ee a
xCerithium variabile (Desh.) ...... Jeol Wt hl (ae Sal dies Salhi x %
[*] submarginatum (Hd. MS.),
var. recentior (d’ O7b.)..........+. se erie (eae? “ie x
pseudocinctum (d’ Ord.) ...... Bee |e he Seem * | *
—-— duplex (Sow.) .........sesseeees ei okey
parvulum (Ed. MS.) ......... ee! 3
—— pliciferum (Ed. MS.)......... Seen sete: «oe
ventricosum (Sow.)..........45 x | * | x
subeonoideum (Hd. MS.) ...| ... x
—— contiguum (Desh.)? ......... seul 3
—— multispiratum (Desh.) ...... {Pesto [bre |
—— gyrostoma (Hd. MS.) ......+. sacl 1%
concavum (Sow.) ....sseeeee {SSG al, 9625]. 5 ewer
yertenisn (HG IMS.) ...030000.% [eee edh ae 9.
Melania fasciata (Sow.) .........66 eam sein! 236 |; *
MUA (SOW.)\ 0. se0cererees [read ce eel ee ae
x-—— brevicula (Hd. MS.) ......... %
*xHydrobia anceps (Wood) ......... x x | %
— Dubuissoni (Bowillet), var.
petit (Hd. MOS.) ccacscsscceeees *
bulimoides (Hd. MS.) ...... he | Gel A |
Melanopsis subfusiformis (Morr.)| * | * | * % x
masitormis (SOW.) ..<.2..--.9 x |K.T.| x ae *
Scalaria levis (Morr.) ..........0.008 saekip ae Wh Se
tessellata (Hd. MS.) ......08. seal pete “esters e 3
Nematura parvula (Desh.) ......... x (KAD) | oe. LN Gate
—— pygmea (Forbes) ............ Wee, oceed eles: |
lubricella (Brawn) ...........- | *
Cecum Morrisii (Hd. MS.) ...... | aaceail ae
Trochus pictus (Hd. MS.) .........) * | | | |
*Trochita (Infundibulum) trochi- | | | |
formis (Lam.) =obliqua (Sow.), ... | ... jy seo Kea x |
Phorus cretifer (Hd. MS.) ......... K.T.| *
Teinostoma minutissimum (Ed.
MMe rasa casas cvvcnceoseesseeses ces leeooe| | eas
Carried forward....... 25 | 46 | 47 | 384 | 33 | 26 | 44 | petal
Q.J.G.8. No. 146. K
118 H, KEEPING AND EB, B. TAWNEY ON THE BEDS AT
Fossils of Middle Headon series, &c. ee
ee Heapon.
a ae |
+ | 5
2) a
BS
ro |
5 | 6
|
Brought forward ............ | 20 | 46
Teinostoma micans (Hd. MS.)......! ... as
iINerita aperta(Sows ners cee: x |K.T
[estuarina (Hd. MS.)|=N.
Zouellai US: OOd) iene eeesseee seen * |K.T.
Neritina concava (Sow.) ......066...! * |K.T
[x]Rissoa carinata (Hd. MS.), var.
denticulata (Hd. MS.)............ Hear ae
ditropis (Hd. MS.)............ | *
Tornatella Minato mis (Sandb.).| x
alteran(WDeS/9) aa asensnese she
| dactylina (Desh.) ............ sas
| % simulatum (Sow.) ............ a5
| Adeorbis apertus (Hd. MS.) ...... *
zstuarinus (Hd. MS.) ...... | % |
| xOrthostoma crenatum (Sow.)...... haa
| --——retiarium (Hd. MS.) ......... ieee
xRingicula parva (Hd. MS.)......... a a
Bulla estuarina (Hd. MS.)......... x | x
lopvaney ye sain (SLAIA)) Snooeensosse
| —— curta (Hd. MS.) .....0......0.-
simillima (Hd. MS.) |e y
PeSCUATIMA ||| Pesce uneaceR cents a
% attenuata (Sow.) ......scc0cce00| e+
navella (Hd. MS.) ..........+. ire
Sowerbyi (Wyst) .......0.02.06- hase
; —— tenuicula (Hd. MS.) ......... | *
| # elliptica, (Sow:)it accrneesseeecl | x
Cylichna globulus (Hd. MS.)...... S00
OyeH NS (Cte, AHISE) Gcadaccoobocass Laas
Dentaliumyyspie suede cece coos
xAnomia tenuistriata (Desk.) ...... Ls soe tee
Ostrea velata (8. Wood) ............ x |K.T
*——- flabellula (Lam.) = venti-|
| labruna (Goldie) merece cee Urea es
| Pecten belli aeeee (S. Wood) . ae
xAvicula media (Sow.)............-+-- Nes
xMytilus affinis (Sow.) ............... \K.T.|
Modiola Nysti (Kieh/, MS.) ...... a
demota(HaiS)) nee f
sod ea biangula (Lam,) .)0...2.0.2---- He |
appendiculata (Sow.) ......... one! sede
ata (OGtL0) cctenvacncan leeseuellin ase
* duplicata (Sow.)=sulcicos-
Lata GING/SE) ilar cies cia rate awiane CHOIRS,
| ¥Trigonoccelia deltoidea (Lam.) .... #* | *
Nucula headonensis (forbes) ...... [ae
Carried forward...... | 41 | 56
Colwell Bay.
* ss
a
Upper
Brockenhurst |BaAqsHort.
beds.
2 4 bre)
| 2) oe
a [3 =) r= bend
ey oS Sl | ce!
ra) SS ures) Oo =|
ZS || a S iS &
a | | oe eae
34 | 38 | 26 | 44 La
| +
se 2 Gr
Ke a ee
%
coe CS *%
. |K.T.
K.T.
Pre goad be
Kea %
pan OM Weiner |. oe
cinco (RG FIDA eel lero
3 ECA areca ee
1 Hes *
6 % ea
39 | 45 | 31 | 57 14
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT.
119
Fossils of Middle Headon series, jc. (continued).
Mippirz Heapon.
UPPER
Brockenhurst (Bacsnor.
beds. |
ie B 3
set | Ee Pee lc aa eae Ve ng
eee eee ae
> a | to =| z ee
elelelel2|sla| we
Sele ele ie |e] ee
pal eel tS) | ee |e es) | el ns
Brought forward ............ AL SGP Gl toon aoninclenieon 14
Nucula nudata ( Wood)...........066. weer [Fe Se le
* BUMS (SOW)! 6.2 jcoeacte nsec tordle cea lavaren ol aoe EET
* Lng! (17/12) aan eec ae Ws [baceat | notes Goods
Leda propinqua (Wood) ............| «+ KET ioe Ke Ke:
¥—— minima (Sow.)...ccecceccceceene att 5 OSE Be *
Cardita simplex (Hd. MS.)......... Bad *
paucicostata (Sandb.)=nodi-
Celeb HAWS) ses cy vas ocoed sede ee ens Xe tele oi |i 9e
deltoidea (Sow.) .........c0008. ae oy ESSAI HERG ASSN) Pee alee
orbicularis (Goldf.) ......... Lil Selteta lias «Re
[+] oblonga (Sow.), var. trans-
SENAY MIS.) atcseoes ee stoacsc: Se GOIN Wicca [has alee oe %
———
[*|Crassatella Sowerbyi, var. hanto-
MINEMSIS A CHA s)) osc secvdeerccesss ens
xLucina obesa (Hd. MS.)
CONCAVACDELT.) sss <ceeees cine
—— pulvinata (Hd. MS.) .........
x—— bartonensis (Hd. MS.)
maitiatan(Hid. MS.) ..- csc eceae
Strigilla colvellensis (Hd. M/S.) ...
pulchella (4g.)
Diplodonta suborbicularis (Ed.
M,
@eceeeossons
@eocoee
%
@oereceshoscces
Pooeereesrersose ee SeSoorees 2 2 oe
e@ocvece
AIS: Sep ccaGoa aga GUpee eR EE Eee Eee
xCypricardia pectinifera (Sow.) ...
Isocardia transversa (Nyst)
xScintilla angusta (S. Wood) ......
Lepton nitidulum (S. Wood) ......
ae fomidum (Hd, MS.) ......-..
Cyprina Nysti (He6.)
«Cytherea incrassata (Sow.).........
== — ftumida (Hd. MS.) ..........00
— suborbicularis (Hd. MS.) ...
subelliptica (Hd. MS.)
*
eoceece
, var. serratina (Hd. MS.) MG
eee
M
ww
eee
*
turgescens (Hd. MS.)......... i
—— hantoniensis (Hd. MS.) ...... ore
* Solandri (Sow.), var. attenu-
ERED AVES.) \\..0.000 cscs sonwesses
[*] elegans (Lam.), var. 0
¥—— Suessonensis (Desh.)
ee CS |
Kea
KT: %
ae ‘
a ea
*
~~ |K|laee
x
Pe KE Ke %
Heese IKE Sle %
oe Ad B eau Nh aes
* x IK.T x *
Kea. *
San rd NB
71 | 54} 58 | 34 | 79 17
120 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
Fossils of Middle Headon series, Jc. (continued).
Mippir Heapon.
| UPPER
| Brockenhurst | BaasHot.
| beds.
Ss) 8 | as
= as tl ©
Elo |ts | 6 | eo mene r
‘Shs 16) eS Saar eo S
° OMaS Ss) = Ss £ a
sl men pedapics er i)
Brought forward ............ 51 | 68 | 71 | 54 | 58 | 34 | 79 il
[x]Psammobia compressa (Sovw.), |
var. estuarina (Hd, MS.), and HO] 36 | eat = *
var. arcuata (Hd. MS.) ...... | | |
rudis (Lam.)=solida (Sow.).| -..| * | * | 2 || *
xTellina affinis (Ed. MS.) ......... Looe ldo) cae eg Kee Teme
headonensis (Hd. MS.) ...... [tedees) ara seaaal | | |
sphenoides (Hd. MS.) ...... buresiealey ae gl nse |
Syndosmya colvellensis (Hd. MS.)| ... |... | *
Mactra fastigiata (Hd. MS.) ...... x |K.T| x *
SUSE (73K LUISE) cagaccmaaecoe meena | | *
xMya angustata (Sow.)=M. pro- | | | |
Guctai(HdaViS)\ine eee ence * | x | * |K.TIK.T, *
xCorbula pisum (Sow.).............5- cre fle oe] 05.6 eM eR ;
x Cuspidata (SO) eee sseeeseases % | 3% | a [KOT KO | se
DRAM USER Ve Goeehcos secebeoa <8 acs | cos |e
*Panopza subeffusa (Hd. MS.)...... secre & ae au ae |
sulculosa (Hd. MS.) .........| »» Sees ofomewe |) «88a le eeanl een
*Solen gracilis (S0.) vo .sccwececcwcels m7) |) =} tectell| ucceete Meret teen
Corbicula obovata (Sow.) ......... | gee |. 36. | 3600) 2 een oa cane ae
Cyrena cycladiformis (Desh.) ..7...|| “KOKO es ere ee x
pisuna (Ves) cseewcec eee mca | | |
«Clavagella coronatia (Desi.)rsc.ccecc| seo |) 0 || eo) || enn een Mneeean mE
Gol ditussii(@P i217) ee eee wes. [ewe [oleate alte ter | rea teen Im
Fistularia Heyseana (Phill) ...... coy ld ccewelmene Bee bcc ||) “5?
SED SCENE S\Dporasqoooodobdeoagondpoacnos wae |. sentel Wont | seth een eee gan
Pola Spi msec seca eee rere aera: voee | gee o| eet aeee | Aeeean eeeaa Mie
Peredo,; Sp.. :.s.c0ieadecesubecsensessscn|aese: ic ve,1| soe Meee al iNeeens ene
Serpula; (Spungen ee eearee [te23)|| 220 || see | 208 K.T.|
Pollicipes reflexus (Sow.) ......... lees jee |
*Balanus unguiformis (Sow.) ...... coe fSGMts) Sone CGI, | x
Callianassa Baylii (Woodw.) ...... pape UG bohe ee IU C oT | |
Solenastrzea cellulosa (Dune.). ...| ... |... | «-» |)... (KOE) 2.5
IEG soon (YG) sococoneoner cae ode? W abe al coe shel Re ae Ieneo |
Reussi CD 21c)) Were eee | see | ewe of dere leess Rect leet oe
gemmans (Dune) ae.2..-- + Jo sicee Hew |/celees | (teri Gel eee
—— Beyrichii (Dune.) ............ ccs Peace |leosc || obo | cco | cos |
granulata (Dunce.) ..........+: | see i) sSe-oi) swine |e eee ee
Balanophyllia granulata (Dune.)..|.... |... |... |-s-- | cee.
Mendropliviliale see serra eee |
Eobopsammia granulata (Dune:).-| ...%| 22.0) ee. secon eee nee
Titharzea brockenhurstii (Dunc.)..| ... | ... |... |... [KAT] ... | # |
Asxopora) Michelint (Dwne.)-.2cc0| ss-+ |. se | =e ecen eee eee
Madrepora Solandri (Defr.) ...... wes | ‘aveaili Mee) eee cal aleeyeen eee Ie
Roemer (Ya7es)) wos seen Kern Recs eoreilscs | cos | 8
amelical(27e>)\iacsecceasascess wos: |: wales | Me se 0 eet ENGIN s IRterereial
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 121
Notes relating to Divergences from Prof. Judd’s lists of Fossils, with
Observations on the Edwards Collection of Middle-Headon Fossils.
Marginella simplex is not in the Edwards collection as from
Barton ; this and the following ten species, viz. Mytilus strigillatus,
Borsonia sulcata, Nematura parvula, Trigonocelia deltoidea, Lucina
obesa, L. concava, Cardita oblonga var., Cardium obliquum, Scintilla
angusta, and Panopea subeffusa, are given in one list as occurring in
Barton beds; and in the other list this range is denied to them.
The range into Barton or Bracklesham beds (as shown by the
Edwards collection) has been overlooked in the case of many species
(viz. twenty-two) in the lists of Colwell-Bay and Brockenhurst
fossils (op. cit. pp. 153-156).
Voluta depauperata (Sow.) has been cited in error by Forbes from
Colwell Bay ; it occurs only in Barton or Bracklesham beds, and is
therefore omitted from our list. V. spinosa (Lam.), type, occurs in
Barton and Bracklesham beds; the form from Brockenhurst and
Middle-Headon localities might be recognized as a distinct variety.
V. tereticosta (Kd. MS.) is plainly only a variety of V. geminata
(Sow.) in which the coste are a little less spiny; all intermediate
degrees occur.
Clavella longeva, var. egrequt (Beyr.). Von Konen mentions
this from Brockenhurst; but we find the absence of ridges as rare
as in Barton examples, and therefore omit the varietal name.
Hippocrenes ampla (Sow.) is not in Edw. coll. from Headon Hill
or Hordwell ; and we consider it does not occur there.
Murex seadentatus, var. cinctus (Kd. MS8.), is labelled in Edw. coll.
as from Barton; but we suspect this to be inerror; it appears to be
from Colwell Bay, as in Prof. Judd’s lists.
Natica obovata (Sow.) occurs at Bracklesham, as shown by the
Edw. coll. WV. grossiuscula (Kd. MS.) is probably only a variety of
NV. Studer, as transitions exist between them. NV. dubia (Kd. M8.)
we consider only a large variety of NV. lamellata (Lam.). NV. epi-
glottina (Lam.) is in Edw. coll. labelled as from Hordwell; we
found it at Roydon.
Cancellaria elongata (Nyst) is in Edw. coll. from Headon Hill
and Hordwell, and C. muricata from Hordwell. C. roydonensis
(Kd. MS.) seems a doubtful species. :
Cerithiwm pyrgotum (Ed. MS.) we consider a Lower-Headon form,
and omit it therefore. C. varians (Kd. MS.) isin Edw. coll. from
Headon Hill. C. cavatum (Kd. MS.) may be only a variety of C. con-
cavum ; both it and C. speculatum (Kd. MS.) occur only at Long
Mead End, and should be omitted from the list. C. ventricosum
(Sow.) is in Edw. coll. from Colwell Bay; C. subventricosum (Kd.
MS.) and C. deperditum? (Lam.) in Edw. coll. seem to be worn
specimens of C.. ventricoswm; we agree with Prof. Judd in omitting
them. C. marginatum (Kd. MS.), var. recentius (d’Orb.), occurs as
in our list; its title to a distinct specific appellation seems doubtful.
O. (Vicarya) concavum (Sow.) is in Edw. coll, labelled as from
122 H. KEEPING AND E, B. TAWNEY ON THE BEDS AT
Colwell Bay. C. trizonatum (Morr.) is in Edw. coll. from Hordwell
&c.; it would therefore seem to be Lower Headon as well as
Upper. C. subconordeum (Kd. MS.) seems doubtfully a distinct form.
C. estuarinum (Kd. MS.) as from Hordwell, in Edw. coll., is founded
on a minute fragment, and we do not insert it. C. headonense
(Hd, MS.) is in Edw. coll. from Headon Hill; but we do not insert
it, as it may be Lower Headon only. C. pulchrum (Kd. MS.) is in
Edw. coll. as from marine Headon beds of. Hordwell. C. pseudo-
cinctum (d’Orb.) is in Edw. coll. as from Barton.
Lurbonilla plicatella (Kd. MS.) is in Edw.:coll: from Roydon only ;
T. plicatilis (Kid. MS.) is there as from Colwell Bay.and Barton.
Melania brevicula (Kd. MS.) is in Edw. coll. as from Hordwell
and Barton; M. Woodi (Kd. MS.) from Hordwell seems a Lower-
Headon shell, and is not inserted; the names M. conica, M. polygyra,
M. minima (Sow. ),we could not ‘find represented in the Edw. coll.,
and omit them.
fiissoa carinata (Kd. M8.) occurs at Barton, but. not the var. cden-
ticulata, according to the labels in Edw. coll.
Conorbis dormitor (Sol.) and C. procerus (Beyr.) occur at Barton,
but not the special varieties to which MS. names are anes in the
Kidw. coll.
Hydrobia polita (Kdw.) from Headon Hill is Upper Hesnal only,
and therefore omitted; H. anceps (Wood) is in Edw. coll. as from
Hordwell, Colwell Bay, Long Mead End, and Barton; H. Dubuis-
soni, var. rimata (Ed. MS.) is labelled as from Hordwell marine bed.
Trochus pictus (Ed. MS.) is in Edw. coll. from Hordwell ; it is in
the Woodwardian museum from near Setley Common, Lymington.
Melanopsis ancillaroides (Desh.) was in Edw. coll. subsequently
labelled MZ. subfusiformis (Morr.) ; the former name may be omitted.
M, subulata (Sow.) occurs twice in Prof. Judd’s list, and with diffe-
rent ranges. MZ. swbcarinata (Morr.) is in Edw. coll. as from Bem-
bridge and Hordwell marine bed; at the latter locality it probably
came from Lower Headon (freshwater) to judge from the aspect of
the shell.
The species of Adeorbis in Edw. coll. are founded on single indi-
viduals ; A. estuarina (Kd. MS.) we could not find.
Orthostoma crenatum (Sow.) is in Edw. coll. from Brockenhurst
and Barton.
Tornatella altera (Desh.) is determined from a single individual
in bad preservation, and seems to us very doubtful. 7’. hinnefor-
mis (Sandb.) [ste] of the Brockenhurst list 1s the same shell as
Acicon limneiformis (Sandb.) of the Headon-Hill list; it is in
Edw. coll. as from those two localities. A. stimulatus is inserted on
the faith of our own researches. A. dactylinus (Desh.) is in Edw.
coll. from Colwell Bay ; we have found it there also.
Rtingicula ringens (Lam.) occurs only in Barton or lower beds.
Trochita obliqua (Sow.) was described originally as “a small but
perfect specimen from. Brakenhurst [sc], in Sussex ; the species is
found much larger in the: cliff at Barton ;” the type was only 1 ineh
long, and was recognized by Sowerby as occurring at Barton, “while
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. I 5S
at Brockenhurst it would have been found in Bracklesham beds
probably ; we consider it a young example of 7. infundibuliformis
(Lam.). We do not know why Edwards should have referred
Brockenhurst forms to a different species from the common Barton
species: we have compared numerous examples both from Brocken-
hurst and Whitecliff Bay, and consider them identical with Lamarck’s
species ; we therefore rank 7’. obliqua as a synonym.
Nerita estuarina (Ed. MS.) seems identical with 1. zonula (8.
Woo
Be pha neritopsidea (Kd. MS.) is from the Upper oe we
therefore omit it.
Ostrea flabellula (Lam.) is in Edw. coll. labelled as from “ Col-
well Bay or Headon Hill” [sic], but in error; the specimen has
evidently come from the Barton Clay. O. ventilabrum is not in
Edw. coll. from Colwell Bay, and it does not occur there; we are
not sure that the distinctive differences given by Mr. Searles Wood
between this species and O. flabellula are constant ; we have com-
pared examples of this oyster, so common in the Brockenhurst bed
at Whitecliff Bay, with other examples from Barton beds; and
some we consider perfectly identical with Barton and Bracklesham
forms.
Avicula media (Sow.) is not in Edw. coll. as from Hordwell or
Headon Hill, but from Long Mead End, 7. e. probably from the
Beacon Bunny (Barton) beds.
Dreissena Brardii (Fauj.) is in Edw. coll. from Hamstead and
Hordwell (Long Mead End), ranging thus through all the fresh-
water series. It occurs in social groups. We found a single derived
specimen just above the Lower-Headon boundary at Whitecliff Bay.
Anomia tenuistriata (Desh.) is in Edw. coll. labelled as from
Barton, Brockenhurst, and Hordwell; if the Brockenhurst example
is to be identified with A. Alcestiana (Nyst), probably the Barton
ones are so also. We follow Edwards in considering them all one
species.
Mytilus strigillatus (Wood) in Edw. coll. is only from Barton
beds; we therefore omit it. M. affinis is abundant at Colwell Bay,
and ranges up from Barton beds.
Nucula semilis (Sow.) is in Edw. coll. only from Barton beds ; we
found one imperfect specimen, however, at White Cliff Bay in the
Brockenhurst bed. NV. lissa (S. Wood) is said by Mr. Wood to oecur
at Brockenhurst; but it is not in Edw. coll. as from there; the
Hordwell examples are possibly from the Upper Bagshot Sands.
Arca appendiculata (Sow.) and A. levigata (Caill.) are in Edw.
coll. as from Barton and Bracklesham beds. .
Cardita deltoidea (Sow.) is not in Edw. coll. from Colwell Bay ;
and we doubt the fact of its occurring there.
Incina Menardi (Desh.), as so determined, is not in Edw. coll.
L. gibbosula (Lam.) and LZ. pratensis (Kd. MS.), in Edw. coll. as
from Long Mead End, are not from Headon beds: we therefore
omit them. JZ. obesa (Kd. MS.) and Z. inflata (Kd. MS.) are in
Edw. coll, as from Barton beds; the former is not distinguishable
124 H, KEEPING AND E. B. TAWNEY ON THE BEDS AT
from those labelled Z. concava; indeed Edwards admitted it as
doubtfully distinct.
Diplodonta obesa (Kd. MS.) exists in Edw. coll. from Barton and
Bracklesham beds. D. dilatata (Sow.), determined as such, is not in
Edw. coll. ; Dixon cites it from Bracklesham.
Strigilla colvellensis (Kd. MS.) we found to be not unfrequent at
Headon Hill. S. pulchella (Ag.) is in Kdw. coll. determined from
a single imperfect valve: it is impossible to say whether it is a
second species ; and we therefore omit it.
Cardium Edwards (Desh.) is not in Edw. coll. from Brocken-
hurst; it is'a Bracklesham shell.
Cytherea suborbicularis (Kd. MS.) we found at Colwell Bay and
also in the Brockenhurst zone at Whitecliff Bay. C. swessonensis
(Desh.): under this name we find in Edw. coll. Barton and Lower-
Kocene shells usually referred to C. tenwstriata (Sow.); we have it
from the Brockenhurst zone in Whitecliff Bay. C. partemsulcata
(Ed. MS.) is from Long Mead End only; we therefore omit it.
Cyprina scutellaria (Desh.) is solely from Lower-Hocene locali-
ties. OC. Nystt (Héb.) is the only species from Brockenhurst in
Edw. coll.; we have it from Whitecliff Bay.
Psammobia compressa (Sow.) is in Edw. coll. from Barton; the
var. arcuata (MS.) is from Roydon and Brockenhurst; and var.
estuarina (MS8.) is, according to the labels, from Hordwell, Colwell
Bay, and Roydon. We have compared these examples, and cannot
see any valid differences; we consider them all one species.
Sanguinolaria Hollowaysuv (Sow.) is not in Kdw. coll. from Lynd-
hurst, but is a Bracklesham shell. The Geological Survey cite it in
error from Middle Headon beds of Whitecliff Bay.
Tellina corbuloides (Kid. MS.) in Edw. coll., from Colwell Bay, is
a crushed specimen, undeterminable, but probably not the Hamstead
species; we omit it. 7’. ambigua (Sow.) is in Edw. coll. labelled as
from Hordwell, but is probably not from Middle Headon beds,
although Forbes cites it from Colwell Bay. 7. reflewa (Kdw.) is a
Bracklesham shell, and does not occur above the Upper Bagshot of
Long Mead End. 7. headonensis (Edw.)is in Edw. coll. from Hea-
don Hill and Colwell Bay. TZ. sphenoides (Kdw.) is from Colwell
Bay. 7’. affinis (Kd. MS.) is in Edw. coll. from Brockenhurst and
Barton ; we found it also at Whitecliff Bay.
Syndosmya colvellensis (Kd. MS.) seems founded on a single
minute valve.
Scintilla angusta (Kd. MS.) is from Colwell Bay, Hordwell, and
Barton beds.
Mactra fastigiata (Kd. MS.) which occurs abundantly at Headon
Hill, is from Hordwell in Edw. coll. M. jilosa (Kd. MS.) from
Colwell Bay and Long Mead End (Upper Bagshot) we are unable to
consider a separate form, so rank it as a synonym.
Solen gracilis (Sow.) is in Edw. coll. from Brockenhurst and Bar-
ton beds.
_ Mya angustata (Sow.) was originally found by Prof. Sedgwick at
Colwell Bay; Edwards has an apparently identical shell which he
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT. 125
at first identified with Sowerby’s species, but subseqnently altered
to M. bartonensis (Ed. MS.) ; we cannot, however, see any distinc-
tion between these and M. producta (Kd. MS.) from Colwell Bay ;
we consider them all one species. Mr. Searles Wood doubts the
Hamstead form M. minor, Forbes, being a distinct species either.
Corbula pisum (Sow.) is not in Kdw. coll. from Headon Hill or
Hordwell; and we doubt its occurrence there; it is, however, fairly
abundant in the Brockenhurst zone of Whitecliff Bay. C. mtida
(Sow.) is in Edw. coll. from Roydon and Long Mead End; it was
originally described from Prof. Sedgwick’s specimens brought from
Middle Headon beds. C. fortisulcata (Kd. MS.) we consider merely
a variety of C. pisum; we omit it, since it comes from Long Mead
End, probably from Barton beds. C. jicus was found at Brocken-
hurst by one of the authors, and is now in the Woodwardian Mu-
seum.
Panopea corrugata (Sow.) is, according to the Edw. coll., only a
Barton and Bracklesham shell ; but quite possibly P. subeffusa (Hd.
MS.) is not really separable from this species; in either case one of
the names must be omitted.
Cyrena subreqularis (Kd. MS.) seems to pass into C. obovata (Sow.).
C’, deperdita (Lam.) is in Edw. coll. from Headon Hill and Barton ;
it is probably from the Lower Headon. C. arenaria (Forbes) in
Edw. coll. is scarcely separable from the preceding; it is from
Headon Hill and Hordwell, but apparently from Lower Headon.
Mr. Searles Wood figures a different form as Forbes’s species. C.
gibbosula (Morr.) is scarcely a distinct form. C. estuarina, C. alti-
rupestris, C. obliquata, MS. names in Kdw. coll., are not inserted ;
' they may probably be Lower-Headon shells.
Balanus wnguiforms (Sow.) we found as frequent at Headon Hill
as at Colwell Bay.
Pollicipes reflecus (Sow.) is cited by Forbes from Colwell Bay.
Callianassa Baylii (H. Woodw.) we have from all the zones of
the Middle Headon.
EXPLANATION OF PLATE V.
The figure represents the coast-section from Headon Hill east of Heather-
wood Point to Cliff End, Colwell Bay ; it passes inland at Warden Point
to avoid the projecting promontory. An attempt is made to represent
where beds may be seen iz situ, and where they are concealed by fallen
material. Notwithstanding that the vertical scale is more than double
the horizontal, it is impossible to show much detail; and for this refe-
rence is to be made to the accompanying vertical sections (pp. 91, 98, and
103).
The bends of the coast-line are approximately indicated by the com-
pass-bearings given,
DIScuUssIon.
The Prestpent remarked that the paper was one of great impor-
tance. The question at issue was one sharply defined but difficult
to come to a conclusion upon without visiting the sections.
126 H. KEEPING AND E. B. TAWNEY ON THE BEDS AT
Rey. O. Fisuur said he had visited the locality with Mr. Tawney’s
paper and sections in manuscript, and that he agreed with the
authors’ conclusions. He thought the error on the part of Prof.
Judd might have proceeded from the fact that at the N.E. corner
of Headon Hill the Middle-Headon fossils were found by the
sea-shore; these, however, were not truly im situ, but had been
brought down by aslip; this he thought possibly the key to the erro-
neous interpretation. In confirmation of the view that the Colwell-
Bay and Headon Venus-beds are one stratum, he had found it with
its fossils in Totland brick-field, near the Hotel, exactly where it
should occur to connect the disjoined portions. He had worked
personally at the Brockenhurst locality at Whitley Ridge, and had
identified the bed at the base of the Middle Headon in Whitecliff
Bay. Consequently, if the Brockenhurst bed is to be called Oligo-
cene, the Middle Headon can no longer be called Eocene.
Prof. Jupp said that the paper rested largely on assumptions. His
method of work in the field and in the museum had been made a
matter of assumption. He had not hastily arrived at his conclusions,
but for twenty years he had worked on these British beds, and for
twelve years had studied their continental equivalents and collec-
tions of fossils made from them. ‘The series of Kocene and Oligo-
cene strata in Western Europe is perfectly clear; but when we
come to Britain a difficulty has always existed. This confusion was
removed by distinguishing the zone of C. concavum from the Broc-
kenhurst series. ‘The authors’ sections were supposed to support
those of the Survey; he thought on examination they would not do
so. The mistake had really originated from using Cytherea encras-
sata to fix the so-called “ Venus-bed” of fossil-collectors—the fact ~
being that that shell has a wide range, and there is more than one
‘‘Venus-bed.” In asserting that the different ‘‘ Venus-beds” are
upon the same horizon the authors begged the whole question. This
autumn he again visited the island, and found that an excavation had
been opened by the authors in a Venus-bed in Totland Bay, but
in one quite different from that in Colwell Bay. Had the authors
searched the Headon cliff they might have found other Venus-beds.
The authors had confirmed his own conclusion that the Headon-Hill
sands do not occur in Totland Bay; and this is fatal to their reading
of the section. As regards the paleontological evidence, he thought
that the method of comparison of most abundant fossils was often
misleading, as might be shown in the case of the Cornbrash and
Ragstone of the Lower Oolite. The authors say that the Brocken-
hurst bed is not above but below the Venus-bed. Now the former is
the equivalent of the Tongrian beds of Belgium; and foreign geolo-
gists all regard the zone of C. concavwm as the top of the Bar-
tonian—that is, of the Kocene. Hence the result of their interpre-
tation of the section was to place beds with an Upper-Hocene fauna
above those containing a Lower-Oligocene fauna.
Mr. Starxrz Garpner said he had always thought that in the
particular section under discussion there was only one Venus-bed :
the section of Headon Hill till last year had been fairly clear; and
HEADON HILL AND COLWELL BAY IN THE ISLE OF WIGHT.” 127
he had never seen more himself. He thought ‘“‘ Upper Eocene” and
“Oligocene” equivalent terms, and the question, which should remain
in use? one of priority.
Mr. Wuitaxsr said that cliff-sections in soft beds were apt to
vary from time to time, so that observers who saw them under
different conditions of exposure were likely to differ in inter-
preting them. The examination of other parts of the island,
and especially the mapping of limestones or other well-marked
beds, might. partly help to settle the question in dispute. Perhaps
the Geological Survey map had been constructed rather too much
on theoretical grounds.
The PresrpEnt said that on the one hand we had the minute
measurements of Messrs. Keeping and Tawney, and, on the other,
the wider views of Prof. Judd. At any rate these views were now
on both sides well laid before the Society ; and the question, although
a difficult one, as he had himself found in working over the ground
25 years since with Dr. Wright, would be now carefully examined
by many others.
Mr. Tawney said that he thought Von Konen, in 1864, had rightly
correlated the German and English beds. As for Mr. Whitaker’s
remarks, he thought a person who was puzzled by a clitf-section
would make but little of a drift-covered country where no sections
were to be seen. He still denied what Prof. Judd had said about
there being more than one marine series. The Certthiwm concavum
zone of Prof. Hébert at Hordwell did not occupy the position attri-
buted to this zone by Prof. Judd in Headon Hill. He maintained
that there was but one Venus-bed. The 6-inch Ostrea vectensis bed
in the Bembridge beds could not be confused with the Middle-Headon
Venus-bed.
(QS0a0" P. H, CARPENTER ON TWO NEW CRINOIDS FROM
10. On two new Crrnorps from the Upper Cuarx of SovTHERN
Swepen. By P. Herpert Carpenter, Esq., M.A., Assistant
Master at Eton College. Communicated by Prof. P. Martin
Duncan, M.B. Lond., F.R.S., F.G.S. (Read February 2, 1881.)
[Puare VIL]
Tux large work* of Prof. Geinitz on the fossils from the valley of
the Elbe in Saxony contains a description of a small stalked Crinoid
from. the “ Pliinerkalk’’ of Strehlen that has long been known to
contain stem-joints of the type to which d’Orbigny gave the name
Bourgueticrinust. Although no calyx was ever met with, the
characteristic stem-joints were supposed to be sufficiently indi-
cative of the presence of the common JB. ellipticus. Some ten years
ago, however, a singularly perfect specimen was discovered, con-
sisting of a complete stem with radicular cirrhi, and a calyx
on the top of it (Pl. VI. fig. 1). But this calyx (fig. 2) proved
to be totally different in its characters from those of the species
of Bourgueticrinus described by @’Orbigny. In B. ellipticus the
calyx is widest round the basal circlet, and tapers gradually
downwards into the stem, while the outer surface of the radials
has a considerable slant from above downwards and outwards. In
@Orbigny’s other species, B. equalis, both radials and basals,
especially the latter, are relatively narrower and higher, and the
whole calyx, together with the top stem-joint, is almost uniformly
cylindrical ; but in each case the top stem-joint is very large and
relatively higher than that of any Apiocrinus, while in B. ellupticus
it widens considerably from below upwards. Its height may be as
much as or more than that of the basal and radial circlets together ;
and the joints immediately below it gradually diminish in width
until they resemble the ordinary stem-joints.
In the Strehlen fossilt, however, the calyx is widest at its upper
end, around the upper and outer edges of the radials, so that its
diameter diminishes gradually from above downwards (Pl. VI.
fig. 2a). The broad external faces of the radials slope downwards
and inwards; and the basal circlet narrows still more, so that the
diameter of its lower face is less than two thirds that of the upper
surface of the radials (fig. 2b). But the top stem-joint, on which the
calyx rests, only expands a little from its lower to its upper margin,
and its increase in thickness over the one below it is far less marked
* “Das Hlbthalgebirge in Sachsen,” Palzontographica, Band xx. Theil 2,
Ds 1S Sh
oS Histoire naturelle générale et particuliére des Crinoides vivans et fossiles
(Paris, 1840), pp. 95, 96.
¢ Thanks to the kindness of Prof. Geinitz, who has made a second exami-
nation of this specimen, I am enabled to give a slightly more accurate figure
of it than that published by him in the ‘ Elbthalgebirge’ (Taf. vi. fig. 9a).
In the older figure only two joints are represented between the calyx and the
enlargement on the stem. In that given here three joints are shown instead of
two, this later interpretation of the markings on the upper part of the stem
being considered by Prof. Geinitz to be the more accurate one.
O
AN Soe ay
JOUrT. or
+
U
Mintern. Bros imp
ith.
Berean del et
Cc
;OUS
RE TAC
=
Sat
@
deal
if
SWE.D
THE UPPER CHALK OF SOUTHERN SWEDEN. 129
than is the case in Bourgueticrinus. Both it and the joints imme-
diately below it are decidedly smaller than those forming the lower
part of the stem, which is just the reverse of what we find in Bour-
gueticrinus.
Prof. Geinitz was unable therefore to refer this specimen to
Bourgueticrinus, despite the resemblance of its stem-joints to those
of that type; but he supposed it to belong to the genus Antedon on
account of the resemblance of its calyx to that of Ant. Sarsw, as
represented by M. Sars in his well-known ‘ Mémoires pour servir a
la connaissance des Crinoides vivants.’ In the specimens figured
by Sars*, ‘‘the upper end of the stem is not thickened, and the
calyx widens from its base to the upper end of the first radial,” just
as in the fossil from Strehlen (Geinitz Tt). This resemblance is but
an imperfect one, however; for Sars’s specimens were merely the
stalked larvee of Ant. Sarsei, not more than an inch long. In the
later stages of these larvet the uppermost stem-joint or future
centro-dorsal piece of the mature and free Antedon not only becomes
considerably enlarged, so as entirely to conceal the basals, but it
also bears cirrhi. This, however, is not the case with the corre-
sponding joint of the Strehlen fossil.
Prof. Lundgren § has already pointed out that this specimen is
too completely developed to be a larval Antedon like those figured
by Sars; but neither he nor any other paleontologist has referred
it to any definite position among the Crinoids.
The ‘‘Mucronatenkreide” (= Upper Chalk) of Kopinge, near
Ystad, in Southern Sweden, contains a quantity of stem-~joints
(Pl. VI. figs. 3-6) which have been considered as belonging to
Bourguetierinus ellipticus, though no calyx of this species has yet
been found associated with them. Some years ago, however, a
singular calyx was met with (Pl. VI. fig. 7), which was presented
to the Geological Museum of the University of Lund by Herr Rector
Bruzelius, of Ystad, into whose hands it had come. Its discovery
was announced in the ‘Neues Jahrbuch ftir Mineralogie’ by Prof.
Lundgren, who at once recognized its resemblance to the so-called
Antedon Fischert of Geinitz (Pl. VI. fig. 2). It is, however, con-
siderably larger and much less conical; but it has even less resem-
blance than the Strehlen fossil has to the cylindrical Bowrgueticrinus
equalis. During my recent visit to Lund for the purpose of
examining the Comatulw of the Retzian collection, Prof. Lundgren
showed me this fossil, and was kind enough to intrust it to me for
description. For this and for many other acts of kindness I offer
him my heartiest thanks.
For these two fossils, so similar in their general characters though
differing in points of detail, I believe that not only a new genus,
but also a new family must be established. I propose to call the
genus Mesocrinus; for while allied to Bourgueticrinus in the cha-
racters of its stem-joints, it is quite as closely allied to the Penta-
crinidg in the characters of its calyx. The only real resemblance
* Op. cit. pls. v., Vi. T Op. cit. p. 18. t Op. cit. pl. vi. fig. 24.
§ Neues Jahrbuch fiir Mineralogie, i876, pp. 180-182.
130 P. H. CARPENTER ON TWO NEW CRINOIDS FROM
to the Apiocrinide is in the nature of the faces of the stem-joints,
which resemble those of Bourgueticrinus and Rhizocrinus. But
similar joints occur in the larval Antedon and in Platycrinus * ; so
that this resemblance does not go for much, especially when it is
remembered that d’Orbigny speaks of the articular faces of the
stem-joints in the Apiocrinide as being most frequently marked
with radiating striee 7.
On the other hand, Mesocrznus differs from the Apiocrinide as
defined by d’Orbigny and by Zittelt, in the presence of verticils of
cirrhi on the stem, and in the small size of its upper joints.
Further, the central funnel of the calyx (Pl. VI. fig. 7a) is small,
not wide and patent; while the articular faces of the radials are
large, and not separated or barely in contact, but meet one another
along the whole length of their sides, and bear distinct fossee for
the attachment of muscles and ligaments. All these characters are
more or less distinctive of the type of the Pentacrinide ; but Meso-
crinus cannot be referred to that family, as it lacks the petaloid
markings on the faces of the stem-joints.
MzsocrInvs, 0. &.
Calyx more or less conical, composed of five basals forming a
complete ring, and five radials with high articular faces which bear
distinct muscular and ligament-fosse, and are in contact for the
whole length of their sides. Upper stem-joints the smallest. Lower
ones with elliptical faces, the long axes of which are occupied by
articular ridges. ‘The planes of these ridges on the two faces of
each joint are more or less inclined to one another. The joints
may bear single cirrhi, or two may combine to form a node for a
verticil of two cirrhi. MRadicular cirrhi at the base of the stem.
MusocRINvs suEDIcUS, n. sp. (Plate VI. fig. 7.)
The lower part of the calyx is formed by five pentagonal basals,
which are in complete contact laterally, so as entirely to cut off the
radials from the top stem-joint. The lower surface of the basal
pentagon is very concave, with a large central perforation ; but it
is quite simple and devoid of any kind of ornamentation (Pl. VI.
fig. 7b). The radials have very high outer surfaces (nearly twice as
high as the basals), which slope very slightly upwards and outwards.
Their articular faces are also rather high and trapezoidal, with large
muscle-plates standing up around the centralfunnel. The thickened
edges of the two muscle-plates on each radial are separated by a
slight intermuscular notch. The transverse ridge expands into a
large articular surface perforated by the opening of the central canal,
to which it forms a thick rim on all sides. From this surface short
ridges proceed upwards and outwards, separating the large muscle-
fosse from the small ligament-fosse. The dorsal fossa for the
elastic ligament is relatively small, being represented by little more
* A Natural History of the Crinoidea (Bristol, 1821), pp. 34, 75.
t Op. cit. p. 1.
{ Handbuch der Palaontologie, Band i. p. 388.
THE UPPER CHALK OF SOUTHERN SWEDEN. USE
than the pit beneath the transverse articular ridge, around which
is a simple smooth surface.
Size. Height 5 millim., greatest diameter 5 mm., least diameter
4 mm., greatest height of basals 1:5 mm., least height 1 mm., width
3 mm.
As already pointed out by Prot. Lundgren, the stem-joints which
occur associated with this calyx are referable to three principal
types. It is, of course, possible that they belong to anothe™ species
altogether ; but, like Prof. Lundgren, I am inclined to refer both
calyx and stem-joints to one and the same species. ‘The question
cannot, of course, be decided until the Swedish collectors are fortunate
enough to meet with a perfect specimen.
Type 1. Thin circular disks, about 3 millim. in diameter, with
faces perforated in the centre, but without markings of any kind.
They probably belong to the upper part of the stem immediately
beneath the calyx. Both in some forms of Bourgueticrinus* and in
Rhizocrinus the upper stem-joints have simple faces without any
of the characteristic sculpture which occurs lower down the stem.
The thin penultimate joint of Mesocrinus Fischert (Pl. VI. fig. 1)
would seem to have been of this nature; and one can readily
imagine that in the larger WM. suedicus the number of such simple
stem-joints was larger, as is actually the case in Bourgueticrinus.
Type 2. The joints of this, the commonest type (PI. VI. fig. 3.), are
higher, with oval articular faces, the long axes of which are occupied
by transverse ridges. ‘The planes of the ridges at the two ends of
each joint are inclined to one another at angles of from 60° to nearly
90°; and the centre of each ridge expands considerably around the
opening of the central canal into a well-marked articular surface.
A median groove extends along each half of the ridge from the
central opening towards the margin of the joint-face; and short
shallow branches proceed from it on each side so as to cut out the
upper portion of the ridge into a double row of small teeth.
According to Prof. Lundgren these joints vary in size from 3
to 8 millim. in diameter, usually 5 or 6 millim.; and their height
is about equal to their diameter.
Type 3 (Pl. VI. figs. 4-6). Wider but lower joints, the oval faces
of which are much more pointed than in those oftype 2. They differ
very much in the proportion of height to diameter. In the thicker
ones (fig. 4) the expansion of the transverse ridge around the
opening of the central canal is very distinct, and there is a crescentic
pit on either side of it. But these features are much less marked
in the thinner joints, the faces of which are flatter (fig. 5), while the
transverse ridges scarcely expand at all around the central canal.
Some of these joints bear portions of the cirrhus-sockets, as already
pointed out by Prof. Lundgren. As in some species of Pentacrinus,
* This is certainly the case in several specimens that I have examined, some
of which, contained in the University collection at Berlin, were kindly shown
to me by Prof. Beyrich. On the other hand, Quenstedt figures a top stem-
joint of B. ellipticus with a distinct transverse ridge and articular facet on its
under surface (Petrefactenkunde Deutschlands, Band iv. tab. 104, fig. 76).
132 P, H. CARPENTER ON TWO NEW CRINOIDS FROM
two joints contribute to the formation of a socket, and the sockets
are at the ends of the long axes of the two apposed faces, so that
there were two cirrhi at each node, and at least three nodes in im-
mediate succession (fig. 6). The two grooves in the respective
transverse ridges form by their apposition a canal which lodged the
vessels proceeding to the two cirrhi from the central vascular axis of
the stem, and opened at the bottom of each cirrhus-socket*.
In the absence of complete specimens of Mesocrinus suedicus it is,
of course, impossible to determine where these nodes or, rather,
groups of nodes occured in the stem, or even whether a stem of this
character was associated with the calyx under description. I suspect
that the verticils of cirrhi were limited to the wide lower part of the
stem ; but it is not possible to form any opinion as to whether they
were simple cirrhi like those of Pentacrinus, or irregularly branched
radicular structures like those on the lower stem-joints of Rhizocrinus
lofotensis.
Failing direct evidence to the contrary, it certainly seems to me
most probable that the calyx and stem-joints from Kopinge all belong
to one species, which would then differ from dMesocrinus Mischert in
other characters than those of the calyx; for the lower joints of
M. Fischert (P1\. VI. fig. 1) are all much longer than wide, as in
Rhazocrinus, Bathycrinus, and the larval Antedon, and they rarely
bore cirrhi(Pl. VI.fig. 1). In this latter respect Z. swedecus must have
been related to MW. Fischert much in the same way as Lhizocrinus
lofotensis with abundant radicular cirrhi on the lower part of its stem
is related to &. Rawsoni f which had “ very few radicular cirrhi.”
The wide lower stem-joints of MW. swedicus (Pl. VI. figs. 4-6)
have much less resemblance to the corresponding joints of 1.
Fischert than to those of Bourgueticrinus ellipticus, as represented
by @Orbigny ; and they further resemble these last in having the
transverse ridge continuous across the articular face. In B. con-
strictus, however, the ridge is interrupted in the centre, and the
more or less marked excavations in the lateral portions of the joint-
face are connected with one another round the central canal, very
much in the same manner as the two cornua of the grey matter
unite around the central canal of the spinal cord +. ‘This feature is
also distinctive of Rhizocrinus and of the Antedon-larva$; and in
both of these types the transverse ridge is cut up into a double row
of minute teeth. So far as I know, this character has never been
described in any species of Bowrgueticrinus; and Geinitz neither de-
scribes nor figures it in Mesocrinus Fischert, though (as mentioned
above) it occurs in J. swedicus.
* Quenstedt (op. ciz. p. 368) has described cirrhus-sockets on stem-joints from
the White Chalk of Rugen, and has remarked that the grooves in the trans-
verse ridges of these nodal joints are often very distinct; but there seem to
have been more than two cirrhi at each node (tab. 104, fig. 63).
t ‘Zoological results of the Hassler Expedition. I. Hchini, Crinoids, and
Corals,’ Ilustr. Catalog. Mus. Comp. Zool. at Harvard College, no. viii. p. 27.
{ This seems to be also the case in the so-called B. ellipticus from the Hocene
of Traunstein (Quenstedt, op. cit. iv. tab. 104. fig. 82).
§ Sars, ‘ Crinoides vivants,’ pp. 5, 6, pl. ii. fig. 27, and pl. vi. fig. 17.
THE UPPER CHALK OF SOUTHERN SWEDEN. 133
One of the stem-joints of WM. Fischeri which is figured by Geinitz
is very singular. There isa thick articular rim around the opening
of the central canal of the oval-oblong face, as in the lower stem-
joints of MW. swedicus; but the ridge proceeding from this to either
end of the oval is Y-shaped and not simple. Some of the stem-joints
of B. ellipticus and also of Platycrinus levis which were figured by
Miiler * present very similar characters; but I have not found
them in any of the joints of J. suedicus.
The genus Bourgueticrinus is rather in confusion just at present,
all those stem-joints occurring in the Mesozoic rocks being referred
to it that have elliptical articular faces with transverse ridges upon
them, which are in different planes at the two ends of each joint;
and we are unable to classify these joints properly in the absence of
sufficiently perfect specimens of whole individuals.
In any case, however, the so-called Antedon Fischeri and its
Swedish ally have stem-joints closely approximating to the Bour-
gueticrinus type (Pl. VI. figs. 3-6). Nevertheless the calyx is
quite different (Pl. VI. figs. 2 & 7). Seen from the side it has a
certain resemblance to some forms of Millericrinus Miinsterianus,
d’Orb., and of WM. Nodotianus, dOrb. But this resemblance dis-
appears altogether when the upper surface of the calyx is examined ;
for the central funnel of Millericrinus is very large, and the articular
faces of the radials which surround it are wide and low, barely
meeting laterally; while Mesocrinus has quite a narrow central
funnel (fig. 7, a) and relatively high articular faces, which diminish
considerably in width towards their upper ends, but are in contact
for the whole length of their sides. |
On the whole the calyx most resembles that of a Pentacrinus, or
rather of that section of the genus with a closed basal circlet, which
is referred by de Loriol ¢ to Cawnocrinus. Had I either calyx alone
before me, I should certainly refer it to Pentacrinus, among the recent
species of which there is a considerable variation in the proportions
of the different parts of the calyx t. In Carnocrinus, Millericrinus,
Bourgueticrinus §, and Rhizocrinus, the composition of the calyx is
the same. In all these genera there is a closed circlet of five basals,
on which the five radials rest, just as they do in Mesocrinus. But
there are considerable differences among these five types in the nature
of the articular faces of the radials. In Afllericrinus these faces
are very wide and low, and are nearly or quite separated laterally,
while the fossee for the muscles and interarticular ligaments are
usually but shghtly developed ||. In Bourgueticrinus the articular
* Op. cat. pp. 34, 75.
t ‘Monographie des Crinoides fossiles de Ja Suisse,’ Geneva, 1877-1879,
p- 111. See also ‘On the Genus Solanocrinus, Goldfuss, and its Relation to
Recent Comatulz,” Journ. Linn. Soc., Zool. vol. xv.
{ Compare figs. 21 and 23 on pl. xi. of Journ. Linn. Soc. Zool. vol. xv.,
with fig. 3 on pl. vi. of the Popular Science Review, new ser. vol. iv.
§ In some specimens of “ 6. ellipticus” in the national collection at South
Kensington the basals appear externally as small triangular pieces which are
not in contact laterally.
|| According to de Loriol, Millericrinus differs from Apiocrinus in the presence
of an articular facet on the first radials. In the latter genus “leur surface
134 P. H. CARPENTER ON TWO NEW CRINOIDS FROM
faces are much reduced and quite insignificant, while in Rhizocrinus
they are wide, low, and separate, and more like those of Milleri-
crinus, enclosing a wide central funnel.
In both species of Mesocrinus, however, and especially in 7. suedicus,
the articular faces are much higher relatively to their width, are in
contact for the whole length of their sides (figs. 2 a, 7 a), and have
distinct muscle-plates, which stand up around the opening of the
small central funnel. These are largest and best developed in MW.
suedicus, but are distinctly recognizable in Geinitz’s figure of I.
Fischer.
These features are eminently characteristic of the Pentacrinide
and Comatulide, though I have seen no calyx of Pentacrinus which
could be said to be precisely like that of Mesocrinus. But then no
two Pentacrinus-calices that I have seen are precisely like one
another; for they differ very much among themselves, not only in
the relative development of the basals, but also in the shape and
proportions of the outer surface of the radials and of their articular
faces. At the same time it must be remembered that we are only
just beginning to become acquainted with these modifications ; for
neither species nor individuals of living. forms are at all abundant
in collections, much less are they available ;for anatomical investi-
gation. The calyx of Mesocrinus Fischer. (fig. 2) finds its nearest
ally in that of P. Wyville-Thomsoni*. ‘It is in a side view that
the resemblance is most evident, the chief point of difference being
the greater height of the radials and of their articular faces in
Mesocrinus. These features are more marked, however, in P.
asteriay ; but in this species the basals are small, and do not meet
laterally as they do in Mesocrinus. Except in this point the calyx
supérieure ne servait pas de point d’attache” (oc. cit. p. 32). I regret that I
cannot altogether agree with this opinion of the distinguished Swiss paleeon-
tologist, who must have been unfortunate in some of the specimens he examined.
The large concave surface in which the second radials of Apiocrinus rest is some-
times an expansion of what in recent Crinoid#is the dorsal fossa lodging the elastic
ligament. ‘This is well shown in de Loriol’s own figures of the ventral aspect
ot the first radials of A. Meriani (pl. ii. figs. 4a, 5a), and also in d’Orbigny’s
figure of A. Murchisonianus (pl. vi. fig. 7). The central end of this large fossa
is bounded by the transverse articular ridge pierced by the opening of the
central canal ; and rising up from this ridge so as to form a part of the rim of the
central funnel are larger or smaller plates for the muscle- and ligament-fosse.
In some specimens of Aptocrinus in the national collection these fossz are re-
latively large and are separated by a well-marked ridge; but in most species
they are greatly reduced in size, as is also frequently the case in Millericrinus.
In the latter genus the dorsal fossa never reaches the enormous size that it does
in Aptocrinus, and, though it is sometimes relatively large (as in some Comatule),
it is occasionally comparatively small.
I am not prepared to say, however, that no Apiocrinus had the first and second
radials united otherwise than by muscles and ligaments. They must, in some
cases, have been joined by a syzygy, e.g. Ap. Parkinsonti (VOrbigny, pl. v. fig. 6) ;
but such cases are very anomalous; for in the other Articulate Crinoids
syzygial union, though common enough between the second and third radials,
never takes place between the first and second. Hyen in Marsupites there is a
distinct articular facet on the first radials.
* Journ. Linn. Soc., Zool. vol. xv. pl. xi. fig. 23.
t Journ. Linn. Soc., Zool. vol. xy. pl. xi. fig. 21.
THE UPPER CHALK OF SOUTHERN SWEDEN. aa
of P. asteria is not unlike that of M. suedicus (Pl. VI. fig. '7), which
has much more resemblance to it than to the calyx of any species
of Millericrinus.
Despite the resemblance of their calices to the Pentacrinus-type,
the so-called Antedon Fischeri and its Swedish ally obviously belong
to another genus than Pentacrinus. They lack the typical stem of
this genus, with its verticils of cirrhi from the top downwards and
the petaloid markings on the joint-faces. Neither does Mesocrinus
possess the typical stem of Apiocrinus or Millericrinus ; but while
chiefly resembling Bowrgueticrinus in the character of its stem, it
differs from that genus and approaches /thizocrinus in the compara-
tively small size of its upper stem-joints; and it especially resembles
ft. Rawsoni in the relatively slight increase in the diameter of its
calyx from below upwards. In neither case does the calyx pass
gradually downwards into the thickened upper end of the stem, as
it does in the typical Apiocrinide and in Bourqueticrinus, to which,
in other respects, Wesocrinus has a considerable resemblance.
The similarity of the articular faces of the stem-joints of the
young Antedon Sarsii to those of Rhizocrinus, and the imperfect
radicular processes that proceed from the lower part of its stem, are
characters which connect the Comatulide with the Apiocrinide.
The Pentacrinide, however, are sharply marked off from the latter
family by the striking differences in the character of the stem. It
is therefore of no small morphological interest to find a type in
which the characters of a Pentacrinus-calyx are combined with those
of a Bourgueticrinus-stem. It is quite possible that some of the
stem-joints now referred to Bourgueticrinus may belong to other
intermediate forms, the calices of which are still unknown to us, as
that of Mesocrinus was but a few years ago.
Prof. Lundgren has been kind enough also to intrust to me the
description of a new Antedon, two specimens of which were found
by himself and by Mr. J. Chr. Moberg in the Ignaberga Limestone
at Balsberg, in the province of Scania, 8. W. Sweden.
ANTEDON IMPREsSA, n. sp. (Plate VI. figs. 8, 9.)
Centrodorsal a thin convex pentagonal disk with very indistinct
traces of a small five-rayed impression at the dorsal pole. In the
larger specimen the dorsal surface is somewhat flattened and tolerably
free from cirrhi (fig. 8), but in the smaller and younger specimen
there is but a very small cirrhus-free space (fig. 9,a). There are
about 40-50 sockets arranged in three rather indistinct rows, with
occasional traces of a fourth; but they are too much worn to show
any structural details.
The ventral surface is entirely obscured by matrix in the larger
specimen, and is only partly visible in the smaller one. It is
markedly concave; and its angles are somewhat produced upwards
and outwards. In the middle line of each radial area is a median
erooye, the central end of which is deepened and forms a radial pit.
The outline of the central opening was probably decagonal; and
L 2
136 CRINOIDS FROM THE UPPER CHALK OF SOUTHERN SWEDEN.
from its interradial sides there proceed five linear oblong basals,
which do not quite reach the circumference. The outer end of each
is marked by an oval oblong impression.
Diameter, larger specimen 8 millim., smaller 5 mm.
Height, larger specimen, 2 millim., smaller 1°5 mm.
Remarks. I do not know of any Comatula, either recent or fossil,
with a centrodorsal at all like that of this species, except Antedon
Tourtie. Schliiter * figures five slight grooves radiating outwards
from the radial pits of this last species ; but he makes no mention of
them in the text. The ventral surface of its centrodorsal is slightly
concave, with the angles raised; but this is far less distinctly the
case than in A. impressa ; and the centrodorsal is half as high as it
is wide, and bears four vertical rows of cirrhus-sockets, characters
which distinguish it sharply from A. impressa. .
The persistence of the basals in connexion with the centrodorsal
rather than with the radials is also interesting. They are probably
the original embryonic basals (or orthobasals), as in A. Lundgreni
and a few other speciest. If they were merely basal rays connected
with a rosette, some trace would have remained of such a connexion ;
but I can find none. |
EXPLANATION OF PLATE VI.
Fig. 1. Mesocrinus Fischeri, Geinitz, sp., natural size. Copied from an
amended drawing of the original, kindly lent by Prof. Geinitz.
2. Calyx of Mesocrinus Fischeri, enlarged: a, side view; 0, dorsal
surface.
3-6. Stem-joints from Kopinge, 8. Sweden, probably belonging to
Mesocrinus suedicus, all X 2: a, face views; 0, side views.
7. Calyx of Mesocrinus suedicus, nov. gen. et sp., X 6: a, veutral
surface; 0, dorsal surface; c, from the side.
8 & 9. Centrodorsals of Antedon impressa, n. sp.: fig. 8. Dorsal sur-
face of the larger specimen, X 4; fig. 9. Smaller specimen, x6:
a, dorsal surface; 6, from the side; c, ventral surface.
Discussion.
The Prestpent expressed his sense of the value of the author’s
communication, and hoped he would continue his work.
Prof. Duncan expressed the same view.
Prof. Srrrey said the variations of Bowrgueticrinus were very
remarkable, both in form and in structure of the calyx. He had
never seen one with the structure of that described, but had seen
some approaching it. He eulogized the description given by the
author, and expected from him important contributions to the
knowledge of the Cretaceous Crinoids.
* “Ueber einige astylide Crinoiden,” Zeitschr. d. deutsch. geol. Gesellsch.
1878, p. 41, Taf. i. figs. 4-6.
t Quart. Journ. Geol. Soc. 1880, vol. xxxvi. p. 550; Journ. Linn. Soe., Zool.
vol. xv. p. 213.
ON A BOULDER OF HORNBLENDE PICRITE. 137
11. On a BovtvER of HorneienveE PrcritE near Prn-y-Carntsioe,
Anetzsry. By Prof. T. G. Bonney, M.A., F.R.S., Sec. G. S.
(Read January 5, 1881.)
Last summer, through the kindness of Professor Rosenbusch, I was
able to examine several specimens of picrite in: the Geological
Museum at Heidelberg, and to study the rock in the field, near the
village of Schriesheim, a few miles to the north of that town. In
September I was walking with some students along the road which
leads out of the village of Pen-y-Carnisiog northwards to Bwlyn
(Anglesey), when I observed, in a field on the left, the fractured
face of a boulder, in which a number of large crystals resembling
augite, glittering in the sunlight, in a dull dark matrix, recalled at
once the characteristic aspect of the Schriesheim picrite. The
boulder had been broken, apparently rather recently, into three
pieces, one much smaller than the other two ; and its volume must
have been not much less than a cubic yard. In its weathered sur-
face and toughness under the hammer it also resembled the Schries-
heim rock. In both, the larger crystals (which are often about
two thirds of an inch long) contain a number of dark serpentinous-
looking enclosures, giving to the cleavage-faces an interrupted lustre
somewhat resembling (except in the absence of a metallic gleam)
that of bastite. The Pen-y-Carnisiog rock looks a little more de-
composed ; but macroscopically the resemblance between my two
specimens is so great that one could believe them to have been
broken from different parts of the same mass.
Part of a Slice from a Boulder of Hornblende Prerite near Pen-y-
Carnisiog, Anglesey. (Magnified 30 diameters.)
sa
ATTAY
4 ip \pbind “
, ym,
Tin BY UALR \ NaN
INS fF SON PAu)
— +S D2 WP IS 1
Mast SON ; Td
< \
a. One of the grains of altered olivine.
6, 6, b. Aggregated small crystals of hornblende, probably of secondary origin.
138 PROF, T. G. BONNEY ON A BOULDER OF HORNBLENDE
When the Pen-y-Carnisiog rock is examined microscopically, the
difference between the two is rather more marked. In it the pre-
dominant mineral is undoubtedly hornblende. This occurs under
three forms :—(a) inumerable small acicular or blade-like crystals,
in irregular tufted groups, forming a kind of ground-mass; these
vary from a pale green tinge to almost colourless, and are generally
very feebly, if at all, dichroic; the comparatively small extinction-
angle shows them to be hornblende (actinolite) ; and there can be
no reasonable doubt that they are of secondary origin; (6) small
crystals, exhibiting often characteristic cleavages and even external
forms (combinations of oP and oP), green-coloured and strongly
dichroic; (c) large crystals (those mentioned above as supposed
augite), including grains &c. of more than one other mineral, to be
presently noticed. Augite occurs not unfrequently in almost
colourless grains and crystals, some of which show a characteristic
cleavage, and, in one or two cases, the characteristic outline (section
of the combination of oP, oP‘, aP%s). The extinction-angle
of the longitudinal sections of these crystals is large, ranging com-
monly from 30° to 40°. They usually occur interspersed in a dull
olive-green serpentinous or chloritic mineral. No olivine can now be
recognized with certainty in the slides; but there are a number of
irregular grains associated in them with the other minerals, and
abundantly included (these being of smaller size) in the large horn-
blende crystals, which there is every reason to believe are pseudo-
morphs after the former mineral. Opacite and rounded crystal-
line grains resembling magnetite abound in these, often clustered
together or lining roughly parallel cracks, which remind us of the
uregular cleavages of olivine; from these a brown staining often
extends inwards for some little distance. ‘The pseudomorphic con-
stituents vary considerably: sometimes, as described above, they
are a brownish or yellowish green, of filmy granular structure, act-
ing upon polarized light, but not greatly changing their colour;
sometimes they exhibit a finely-speckled aspect, as though aggre-
gates of extremely minute grains or folia of a mineral that acts
strongly upon polarized light; sometimes they are aggregated small
folia of a mineral resembling tale; and sometimes a clear isotropic,
or nearly isotropic, mineral, such as is common in ordinary serpen-
tines. Two or three of the inclusions in the larger hornblende
crystals exhibit a radial aggregate structure with the usual black
crosses. Though most of the above microlithic products are not the
most usual replacements of olivine, I have seen them occasionally
in my studies of peridotites, and have no doubt that this mineral
was formerly present in the Pen-y-Carnisiog rock (probably a
rather ferriferous variety). Magnetite is not uncommon as an in-
clusion in the larger hornbiende crystals; the slide also contains a
little altered brown mica, and a few small crystals of apatite.
With regard to the large black crystals already mentioned,
although, from their optical properties, one cannot but regard them
as a brown hornblende, I doubt much whether this is not due to
subsequent paramorphic change, and believe that they were for-
PICRITE NEAR PEN-Y-CARNISIOG, ANGLESEY. 139
merly a true augite. The extinction-angles are generally less than
20°; but in one slide are two crystals which, though dichroic, give
angles of about 30°. The larger crystals of the Schriesheim picrite
agree with augite in their feeble dichroism and general appearance ;
but the results of several measurements of the extinction-angle are
less than 20° in the case of the largest crystal, while in a smaller
one they are over 30°; and a very considerable quantity of horn-
blende, similar to the varieties (a) and (6), is present in the body of
the slide. A little olivine has escaped change; and the structure of
the rest is rather more characteristic. Still, except that a mica is
decidedly more abundant in the Schriesheim than in the Pen-y-Car-
nisiog rock, the main difference appears to me to be, that the latter
has undergone more alteration than the former, so that it, too, has
once been a true picrite.
Another rock is very abundant in boulders in this district of
Anglesey, which, at first sight, has some resemblance to the picrite,
though less porphyritic in structure. Closer examination, however,
shows that felspar is always a constituent of this, though it is often
not very conspicuous. I have examined a specimen microscopically,
and find it to consist of a green hornblende, an altered felspar, a
brown mica more or less changed, apatite, and a chloritic mineral.
The hornblende and felspar are rather irregular in external form: the
latter is almost wholly replaced by microlithic products; but one or
two grains still retain sufficient traces of their original structure to
show they have been plagioclastic. It is somewhat singular that a
rather similar rock, but with more brown mica and better-preserved
felspar, occurs at Schriesheim, within a short distance of the picrite,
also intrusive in the granite. This is named a Labrador-diorite by
the German petrologists.
The only other instances known to me of the occurrence of picrite
in the british Isles are two in Fifeshire, described by Prof. Geikie
in his excellent monograph on the Carboniferous Volcanic Rocks of
the Firth-of-Forth basin*, and one described by myself, to which,
as I had at that time never examined a typical picrite, and had
failed to obtain a very clear notion of the rock from such descrip-
tions as I had seen, I did not venture to attach the name. In this,
however, olivine (still very fairly preserved) is the dominant mi-
neral; so that it comes nearer to a normal peridotite. The rock was
collected many years ago by Professor Sedgwick, near Penarfynydd,
in the Lleyn peninsula; and Mr. HK. B. Tawney, who lately visited
the locality expressly to search for it in sitw, failed to find it, and
believes that the specimen must have been taken from a boulder.
Here also, as described by Mr. Tawney, are olivine-diabases and
hornblendic diabases.
I have ventured to draw especial attention to this Anglesey spe-
cimen, in the hope that some geologist may succeed in discovering
a like rock in situ. As the picrite just described is so uncommon
and of so marked a character, we might assume with much confi-
* Transact. Roy. Soc. Edinburgh, vol. xxix. p. 437.
+ In a paper by Mr. E. B. Tawney, Geol. Mag. Dee. 2, vol. vii. p. 208.
140 . ON A BOULDER OF HORNBLENDE PICRITE.
dence (supposing no physical difficulties presented themselves) the
Pen-y-Carnisiog boulder to have been derived from that parent rock.
This would afford us most valuable evidence as to the direction in
which the agent of transport (doubtless ice) had formerly moved.
The south side of the Lleyn peninsula, even if the rocks corresponded
(which they do not), seems excluded by physical considerations ;
but I may remark that, though I have examined many boulders in
Anglesey, I have failed as yet to identify any of them with rocks .
from the Lake District or from Scotland, and think that we must
look to the mountains of North Wales for the home of those which
cannot be found in Anglesey itself.
ON THE GEOLOGY OF CENTRAL WALES. 141
12. The Gronoey of Cenrran Wares. By Watrer Kezerine, Esq.,
M.A., F.G.S., Lecturer on Geology in the University of Cam-
bridge. With an ApPENDIX on some new Species of CLADOPHORA,
by Coartes Lapwortu, Hsq., F.G.S. (Read June 23, 188U.)
[Puate VIT.]
ConTENTS,
Part I. More distant sections.
Introduction and Historical. (1) Llanbrynmaer area.
Illustrative section from Aberystwyth (2) Dovey ~wallsy area.
to the Devil’s Bridge and Plyn- (3) Corris area.
laniaion. (4) The Cardigan area.
(1) The Aberystwyth Grits. General results.
(2) The Metalliferous-slate Group. Part IIT
(3) The Plynlimmon Group. art 1h.
Paleontological evidence.
Part II. General summary.
Brief notes upon other sections.
(1) Aberystwyth through Pont APPENDIX.
Erwyd to Builth. Appendix by Mr. C. Lapworth, F.G:S.,
(2) Llandeilo to Aberaeron. on new Species of Cladophora.
(3) Rhyader to the Teifi Pools.
General results.
Part I.
Tue following communication contains some of the results worked
out in frequent field-excursions during three years’ stay at the
University College of Wales, Aberystwyth. In many of these ex-
cursions I was accompanied by my students of the College; and to
them I am indebted for much help both in the museum and the
field*. Our principal field of work was, naturally, within a radius
of some fifteen to twenty miles around the town of Aberystwyth ;
and most of this country we have carefully searched and traversed
through and through. The more distant areas to the south of
Cader Idris, at Llanbrynmaer, Llandovery, Llandeilo, Cardigan, &c.,
have also been visited with a view to the determination of the
extent and variation of the Cardiganshire rock-groups, and the dis-
covery of their stratigraphical relations to other and better-known
geological horizons.
Little has yet been done by geologists to elucidate the structure
of this part of Wales: while the most careful labours of our greatest
authorities have been devoted to the study of the northern counties
and eastern borders of Wales, and also, of late years, to the south in
Pembrokeshire, this barren and chaotic area of Mid Wales has been
always neglected, and is even now very rarely touched with the geolo-
gical hammer. For the bibliography of our subject we have therefore
but little to say, the most important contributions being :—the work
* In particular, I have received much assistance from my former pupils
Mr. T. Roberts, now of St. John’s College, and Mr. E. Evans of Sidney College,
Cambridge.
142 WALTER KEEPING ON THE
of our great leader Sedgwick, published in the Society’s Journal in the
year 1847 (vol. ii. p. 150); a slight account of the Dol Fan conglome-
rate, and a description of the Lampeter worm-trails in Murchison’s
‘Silurian System, pp. 316, 317; some scattered remarks by Mr.
Salter and Sir Roderick Murchison in ‘ Siluria, and by the former in
the Cambridge ‘Catalogue.’ The Pont Erwyd district is referred to
in Symonds’s ‘ Records of the Rocks,’ pp. 132,133; some Graptolites
from Aberystwyth are recorded by Mr. J. Hopkinson, F.G.S., in the
‘Journal’ of the Quekett Microscopical Club, vol. 1. p. 151; and
the mineral veins of Cardiganshire are described by Mr. Warington
Smyth, M.A., F.R.S., in the ‘Memoirs of the Geological Survey,’
vol. ii. part 2, p. 485.
The present communication, although worked out in a close net-
work of foot-routes in parts of the district, and cross traverses over
the rest, is offered only as a first reconnoissance report, which must
be followed by many labours betore the structure of this great and
complicated district can be thoroughly mastered. Some general
order amidst the whirl of contortions, however, is now made clear,
such as the general succession of the Aberystwyth, Metalliferous,
and Plynlimmon groups, and the great Plynliimmon synelinal. The
enormous apparent thicknesses of the rocks are shown to be in part
due to a series of inversions; and, further, the interpretation and
correlation of the beds are greatly helped forward by discoveries of
fossils, mostly Graptolites, in a number of localities, which afford
excellent data for comparison with the more distant Scotch and
Cumbrian Silurians.
Even Sedgwick’s work (1846) was but of a very superficial kind ;
for he tells us, ‘“‘ I profess not to know well this most contorted and
perplexing country.” He makes four rock groups, namely the
(1) Aberystwyth, (2) Plynliimmon, (3) Upper South-Wales Slate
with the Rhyader Slate, and (4) Cambro-Silurian groups, which
appear in ascending order from west to east; but he adds, “the
sections are singularly contorted, the groups ill defined, and the
actual order of superposition obscure.” His first group I still main-
tain under the name of the Aberystwyth grits; but nearly all the
remaining rocks in the line of section might, I believe, have been
included in his second great series—the Plynlimmon ‘group. On
the other hand, I have considered this great Plynlimmon group of
Sedgwick under two distinct headings, namely the (inferior) slate
series or Metalliferous-slate group, and the overlying Plynlimmon
grits, so that we now have the following succession of deposits :—
(3) The Plynlimmon grits, forming a line of high country
in the centre of Wales, including Plynliimmon.
(2) The Metalliferous-slate group, forming a broad zone of
Cardiganshire contorted country on each side of (8).
group. (1) The Aberystwyth grits, best developed between Aberyst-
wyth and Aberayron.
Nos. (1) and (2), being closely bound together by their fossils, are known
together as the Cardiganshire group.
For an illustrative section of our area the best I can offer is that
from Aberystwyth, through the Devil’s Bridge, to the Plynlimmon
143
GEOLOGY OF CENTRAL WALES,
Fig. 1.—Section from Aberystwyth to the Devil’s Bridge.
(Horizontal scale, $ ch to a mile.)
Ww. BE.
Aberystwyth. Devil’s Bridge. The Arch,
RAS Zz
PP pos
Vi
S
=
PUG
Aberystwyth grits. Metalliferous-slate group.
The continuous dotted line indicates the probable course of the Cefn Hendre and the Devil’s-Bridge fossil-zone.
.
Fig. 2.—Continuation of the Section in fig. 1, from Owm Ystwyth, through Craig Lluest, to Rhyader and Gwastaden.
(Horizontal scale, 1 inch to a mile.)
W.<—e@ m—>T, W.N.W.<—= Onc
Popty. Cwm Ystwyth. Craig Lluest (about 1200 feet), Pont ur Elan, Pen Rhiev Wen. Gwyn Llyn. Rhyader, Gwastaden,
Za
A
(j---~---+--=-
i
Large-llag series. Grits and paper shales. Pale slate, thin Shaly slates. Hard pale Conglo-
The Plynlimmon Synclinal. grits and shales. slates. merates.
144 WALTER KEEPING ON THE
Mountains (figs. 1 & 2). The lowest beds form the cliffs at the coast,
while the highest go to form the central mountains. All these rocks
are amazingly contorted ; and we find the intermediate or Metallifer-
ous group especially thrown into frequent and violent twistings,
with, in many places, actual inversion. A continuation of the section
eastward, beyond Plynlimmon (fig. 2), shows a similar appearance of
the rock groups in reversed order of outcrop and with contrary dips,
thus showing that Plynlimmon, like its more ancient and greater
fellow Snowdon, stands in a geological valley or synclinal. We
proceed to the detail of this section.
1. The Aberystwyth grits consist of beds of hard, compact, dark
grey grit or greywacke, and dark shales, rabs, and imperfect slates
in strikingly regular alternation, as may be seen in the ordinary
photographs of the Aberystwyth cliffs.
The grey grits or greywackes are of great sameness and regularity
both in structure and composition around Aberystwyth, being hard,
grained rocks, often felspathic, regularly and sharply jointed. A
cross fracture often shows a remarkable contortion in the lines
of lamine, this being, I believe, mostly of subsequent “‘ concre-
tionary” origin; many of the beds themselves are also, in part,
of the same concretionary growth. ‘The beds measure very con-
stantly about 4 to 6 inches in thickness; and their under sur-
faces exhibit an abundance of raised markings, which are irregular
or tortuous, branching, net-lke or worm-like, these being also, in
part, of concretionary origin.
The argillaceous partings are usually of about the same thickness
as the greywacke-beds, sometimes thicker (especially to the east and
south), sometimes thinner (as In many places around Aberystwyth).
Most of their varieties are the result of subsequent metamorphic
changes acting differently upon the rock according to a slight
diversity of original constitution, or depending upon slightly dif-
ferent mechanical conditions. Thus have been produced the various
forms of shivery shale, large platy shale, rubbly rab* of various
forms and sizes, soft shaly slate, and even very well-marked regular
slate in the Aberystwyth district. They are uniformly of dark
colour, and never greatly indurated. Lenticular nodules with ‘‘ cone-
in-cone”’ structure are of frequent occurrence both in this and the ~
following (or Metalliferous) series.
Fossils—Fucoidal and worm-like markings are of frequent and
wide-spread occurrence throughout this series, appearing for the
most part in the form of raised markings upon the under surfaces of
the grits. I have also found Graptolites in several localities.
Quarry at Cwm, on the south side of the Clarach Valley.
Monograptus Sedgewickii, Portt. Monograptus tenuis, Portl.?
—— Clingani, Carr. Buthotrephis, small species.
lobiferus, M/‘Coy.
* A rab is a fine-grained rock, usually argillaceous and not indurated, which
readily breaks up into a rubble of cuboidal or prism-like fragments.
GEOLOGY OF CENTRAL WALES. 145
From the Bryn-y-Carnau Quarry near the old Water-reservoir,
Aberystwyth.
Monograptus tenuis ?
Dictyonema delicatulum, Lapw.
(n. sp.).
But the most important zone of fossils is found somewhat higher
up in the series, exposed in a quarry formerly worked for building-
stone and road-metal, in a field below Cefn Hendre, where we have
collected
Monograptus Sedgewickii, Porél.
, var. distans, Port. —— tenuis, Portl.?
—— Clingani, Carr. Oxthoceras, sp.
lobiterus, M*‘Coy. Calymene.
turriculatus, Barr. |
Monograptus Sedgewickii, Port.
crenularis, Lapw.?
lobiferus, M/‘Coy.
Monograptus Hisingeri, Carr.
Many of these fossils were found in a set of thin, dark-grey, mica-
ceous flags (the large-flag series), which are sometimes to be obtained
of large size (4-6 feet square).
Dips and Foldings.—Many rock-foldings, some of them very
violent and accompanied by fractures, are seen in our line of
section, good examples being exposed near the second milestone
from Aberystwyth ; so that for a mile anda half along the Upper
Devil’s Bridge-road we appear to have only the same set of beds,
repeated again and again by a number of rock-foldings (see section,
fig. 1). But beyond this the easterly dip becomes more constant,
and we appear to be traversing the outcrop of a continually ascend-
ing series.
2. The Metalliferous-slate Group.—In the Cefn-Hendre quarry,
only about a mile and a half east of Aberystwyth, we already find a
larger proportion of shales to grits than in the coast-section around
Aberystwyth ; and this change becomes still more marked in another
quarry on the road-side further on down the hill towards Gogerddan. °
The same gradual though not perfectly regular disappearance of
the grits to the east may be seen in our present section along the
Devil’s-Bridge road, as, indeed, in any other of the east and west roads
from Aberystwyth*.
A change in the character of the argillaceous rocks appears in
regular correlation with the loss of the grits. They become more
and more indurated and cleaved, until, as the boundaries of the
grit-series are reached, the normal cleavage of the district (striking
N.N.E. and 8.8.W.) is found even in the partings between thick
erit-beds. Thus gradually do we enter into the territory of our
second series—the Metalliferous Slates.
The hills of this district are barren and desolate, even more so
than in the Aberystwyth-grit country ; but they are decidedly more
rounded and regular in their contours. Here, in the uplands, is a
* The limit of the grit series may be placed, as indicated by the yellow dots
upon the Survey Map, at about three miles and a half east of Aberystwyth. In
my pocket-book I find “‘at three miles from town, grits fewer and thinner than
at Aberystwyth,” at four miles ‘‘a few grit-beds as much as 6 inehes thick,” and
at five miles “still a few thin grits.”
146 WALTER KEEPING ON THE
vast dreary mountain-region of bare sheep-walks scantily marked
out into districts by poor stone walls and wire fences, with much
waste bog and peat land. The rocks are of uniform pale blue and
grey colours, varying from small papery shales (rarer) to large
irregular platy shale or regularly cleaved slates, also (in some areas)
much indurated small slate rock cross-cut into fragments by frequent
bedding- and joint-planes. Some zones of softer rab, like that of the
Aberystwyth group, and a pale mudstone rab are sometimes found,
especially near the junction with the grit series.
As we reach the central mining district, some seven miles east of
Aberystwyth, beds of hard, pale, indurated slate-rock with frequent
bed-bandings occur; and in the immediate neighbourhood of the
mineral veins such induration is nearly always well marked.
Occasionally a bed of grit, 2-6 inches thick, occurs in this series ;
but such occurrences are very rare, so that the building- and road-
stones of the central ‘‘ Metalliferous” country have to be carried
for miles, either from the Aberystwyth grit quarries in the west, or
from the Plynlimmon group further east.
Thin ferruginous gritty bands, about 4 inch thick, however, are
more frequent, some of them being highly micaceous. Many such
are seen between the fourth and fifth milestones and around the
ninth milestone on the Devil’s-Bridge road.
Rock-foldings.—Several excellent exposures of the contortions in
this slaty series are seen along our line of section. There is a neat
little synclinal at seven miles, an anticlinal towards the eighth mile-
stone; and several folds may be detected about nine miles east of
Aberystwyth; but overriding these foldings the prevailing dip is
seen to be clearly and determinately to the east.
Fossils are rare in this series. The curious branching structure,
Nematolites Edwardsii, Keep., occurs at Ty Llwydd; and I have
found the Fan Algal (Buthotrephis major, Keep.), the Nematolites,
and worm-trails (Werettes) in several other places. But in other
areas, especially at Cwm Symlog and near Machynlleth, out of our
present line of section, a rich Graptolite-fauna has been discovered,
and will be described later on.
The Devils Bridge, great Inversion of the Rocks (fig. 1).—As we de-
scend the hill to the Devil’s Bridge we pass over pale, hard, shaly
slates* with thin gritty bands about 1 inch thick, marked with worm-
tracks (Nereites Sedgwickit), impressions of the Fan Angal (Buthotrephis
major, Keep.), and Nematolites Hdwardsi, Keep. Coarse roofing-
slates have been worked about half a mile west of the hotel. These
rocks belong to the Metalliferous-slate series; but coming to the
waterfall we meet with a set of alternating thin grits and large
pale shaly slates, together with some large flags of laminated grit,
with fossils exactly resembling those already noticed from Cefn
Hendre.
Many of the grit bands are thin and little jointed, so that large
* Although the splitting of these rocks is so irregular and shale-like, yet the
planes of division are of subsequent cleavage origin ; therefore I call them shaly
slates rather than slaty shales.
GEOLOGY OF CENTRAL WALES. 147
flags may be readily extracted, from which feature I have called this
zone the ‘‘ Large-flag series” (fig. 2). The dip is to the west, running
under the slaty series. Fossils may be found here in the open quarry
above the Devil’s Punch-bowl, and along the sides of the waterfall
itself; but all the Dendroid Graptolites (Cladophora) are from a
band above the iron bridge in the waterfall-grounds ; while some
other beds below this bridge are so crowded with Crinoid ossicles as
almost to merit the name of Limestone.
Fossils from the Devil’s Bridge :—
Monograptus Sedgewickii, Port/.? Odontocaulis Keepingii, Lapw.
—— spiralis, Geinitz. (n. sp.).
turriculatus, Barr. Chonetes lzevigatus, Sby.?
Dictyonema venustum, Lapw.(n.sp.). Orthis, sp.
—— corrugatellum, Lapw. (n. sp.). Other fragmentary Brachiopods.
Calyptograpsus (?) plumosus, Lapw. Phacops, n. sp.
n. sp.). Fragments of Encrinites.
Rhizograptus (?) digitatus, Lapw. Nereites Sedgwickii, Murch.
(nu. sp.). Myrianites tenuis, I‘ Cov.
—— ramosus, Lapw. (n. sp.).
Now in this list of fossils the species of Graptolites are seen to
correspond with those of Cefn Hendre, the occurrence of Mono-
graptus turriculatus in both places being an especially important
fact, this being a species of very limited range.
And we have seen that they occur in identical rocks in the two
places; I therefore cannot doubt that these are really one and the
same set of beds, seen in the upper part of the Aberystwyth grits at
Cefn Hendre and reappearing at the surface in an anticlinal at the
Devil’s Bridge. |
This conclusion, however, is in direct antagonism with the strati-
graphical appearances ; for, notwithstanding the numerous folds, the
predominance of the easterly dip is most determined and impresses
itself strongly upon the mind.
Being convinced of these appearances, it was determined to test
the thickness of the beds by actual measurement; and our exact
observations and calculations, made at more than 100 exposures
along the Devil’s-Bridge road from Aberystwyth, strikingly con-
firmed our earlier impressions, giving, indeed, a result of nearly four
miles thickness of strata (3 miles 1612 yards). In such apparent
conflict of evidence, and in the absence of large faults, the only
reasonable explanation is that the original natural order of the
rocks has been destroyed by the formation of a great inversion, or
rather, as I believe, a series of inversion folds in the Metalliferous-
slate series (see fig. 1). And indeed this interpretation, in con-
formity with the fossil evidence, is independently almost demanded
to explain away the enormous apparent thicknesses of similar rock-
beds as measured from their present dips.
We may then safely conclude that in the Devil’s-Bridge rocks we
are again upon the upper part of the Aberystwyth-grit series.
Continuing our section eastward over the hill through the Arch
to Cwm Ystwyth (fig. 2), we still traverse a series of shaly slates of
the “‘ Metalliferous” type, with here and there thin grits apparently
148 WALTER KEEPING ON THE
belonging to the Large-flag series. The presence of Fucoidal mark-
ings, including the Net Algal (Reteofucus extensus, Keep.) and Nema-
tolites at one mile and a half from the Devil’s Bridge, also serves to
indicate our proximity to the Aberystwyth-grit series. The general
apparent dip is clearly eastward, with some foldings.
Descending beyond the Arch towards Kglwys Newydd the only
matter of special interest is the occurrence of a thin seam of rotten-
stone (a decomposed limestone) which may perhaps correspond with
the crinoidal zone in the Devil’s Bridge. Such rocks are of very
rare occurrence in Mid Wales, so that it is a popular saying that
‘‘ there is no lime in Cardiganshire.”
The rocks around Popty, near Eglwys Newydd, are again seen to
be very much of the Devil’s-Bridge type; and I am inclined to think
that a set of rock-folds with reversals have here brought that fossil
zone near to the surface again. We now reach a region of manifest
great rock-foldings; and as we ascend Cwm Ystwyth a number of
exposures display an important westerly fold in the rocks. The
beds appear still to belong to near the junction of the Aberystwyth
grits with the Metalliferous-slate group.
Next we pass through the rich metalliferous district of Cwm
Ystwyth with its network of mineral veins in the Metalliferous-
slate group, beyond which, at Blaen y Cwm, thicker grits (about
2 feet) with east and south-east dips come in amongst the slates;
and these latter become replaced over a considerable area by dark
shaly slate, rab, pencil-rab, and other softer forms of the argillaceous
rocks.
Thick grit-beds, which are cleaved, next form a prominent feature
at Craig Lluest (fig. 2); and these I regard as belonging to the
lower part of our upper grit-series—the Plynlimmon group. This
series is better developed in Plynlimmon itself, to which we must
refer (infra, p. 156) for a more detailed description. The dip is
eastward.
Some three quarters of a mile beyond the top of the pass*the dip
changes, a westerly slope setting in; and this remains well sustained,
though with some east foldings, on to the hills west of Rhyader.
Here, then, we see the eastern half of the great axial synelinal of
this part of Wales—a great fold in which Plynlimmon lies; ‘but
its apparent magnitude is greatly exaggerated by the phenomena
of reversed dips. The lithological details of this part of the section
in its frequent slight variations, but general monotony, till we
reach Rhyader, would occupy much space and be of little value.
Some pale shaly slates approaching the character of the Tarannon
shales, and thin gritty bands, are seen on the dreary bog- and moor-
land of the higher plateau and on the east of the pass, where also
some of the grits exhibit irregular fucoidal markings and the Net
Algal (Retiofucus extensus, Keep.) upon their under surfaces.
One good anticlinal fold in “ Metalliferous slates” with some
erits has its axis about one mile and a half east of Aber Gynwy; and
a synclinal in the slaty series is indicated lower down on the road
to Pont ur Elan. ‘The well-sustained general westerly dip of the
GEOLOGY OF CENTRAL WALES. 149
great series of thin-bedded slate, pale- or dark-coloured, seen in the
ascent from this bridge to the top of the high part of Rhyader,
appears to show these rocks as in regular serial continuity with
the beds passed over on the great slope next to the west, the whole
forming the vast westerly fold complementary to the great easterly
dip of the Metalliferous-slate series between Aberystwyth and the
Devil’s Bridge. And just as the latter is now proved to be not one
continuous series, but reallya much smaller group affected by fre-
quent inversion, so we are, I think, justified in adopting a like inter-
pretation for these beds to the east of the Plynlimmon axis. The
correspondence of the rocks on the two meridional sides of this axis
is further illustrated as we reach the eastern edge of the great plateau
above Gwyn Llyn (fig. 2), where we find a zone of pale banded and
indurated slate rock identical with the Strata Florida slate rock used
in the Aberystwyth stone pier. These pass under a series of grits
and conglomerates in the beautiful valley of Cwm Elan. A little
further south these latter beds reappear in the Gwastaden grits
and conglomerates of the hills east of Rhyader. Thus our accumu-
lated facts support the view that there are two distinct series of
grits in Cardiganshire, separated by the Metalliferous-slate group.
The Rhyader grits and conglomerates appear to be nearer to the
Plynlimmon than the Aberystwyth group.
The Aberystywth Grits, extent, varrations, Jc-—A glance at the
yellow-dotted area upon the Geological Survey Map will show that
the Aberystwyth grits form a crescent-shaped patch of country in
the centre of the western Welsh border, extending from near Borth,
some five miles north of Aberystwyth, to Traeth Bach, south of
Llangrannog, a distance of thirty miles, and with a maximum
breadth, at Mynydd Bach, of nine miles.
A set of characteristic surface-features marks off its boundaries
with tolerable distinctness, its barren or gorse-covered ridgy hills,
elongated along the line of rock strike, and with minor sets of
parallel crests and ledges (sometimes forming sets of small step-
like structures or inclined ribs in the lines of more durable grit-beds),
giving to the group an almost unmistakable appearance*..
The general characters of the rocks have already been described
in our Deyil’s-Bridge line of section; and the variations from those
types are neither numerous nor very striking. The greywacke and
erits are very constant in grain, never becoming conglomeratic; but
some coarser varieties are found in a few localities—for example,
around the Hiddwen lakes, Mynydd Bach, and at Pen Craig, north of
Llanilar. In these places the greywacke is almost granitoid in
appearance, the quartz grains being large, flakes of mica common,
* It was pointed out long ago by Sir Henry de la Beche that the same type
of physical features appears in the area of the grits of Penrhyn ddu in the
Lleyn peninsula, which are marked Lower Cambrian upon the Survey Map.
To me this resemblance also appeared very striking. The Penrhyn-ddu beds
are totally unlike any of the Longmynd group known to me; and I cannot
believe they are of such an age; nor do I think with de la Beche that they are
of the same age as the Aberystwyth beds, but regard them as an exceptionally
developed type of the Tremadoc series.
Q.J.G.8. No. 146. M
150 WALTER KEEPING ON THE
and crystals of felspar, sometimes perfect but more often fragmen-
tary, very numerous and conspicuous. These constituents are held
together in the dark argillaceous greywacke matrix. The rock often
closely simulates a volcanic ash*.
In thin sections, examined under the microscope, the Pen-Craig
rock exhibits irregular angular and subangular fragments of quartz
and felspar, the interstices filled with the dark, opaque (argillaceous)
matrix. The quartz is somewhat cracked, and includes numerous
cavities and minute spicular microliths; these latter are grouped
into wavy stratoid zones, between which the principal cracking of
the quartz runs. ‘The felspar is mostly in the form of.very angular
crystal-fragments, usually much decomposed, and of powdery ap-
pearance; but some of the better-preserved fragments show the
characteristic ribbon banding of the Plagioclase group when ex-
amined with polarized light.
The ordinary finer-grained beds are usually of darker colour than
these, and contain less felspar; they are, however, for the most part
quite similarly constituted, the felspar crystals often being readily
recognizable when decomposed into irony spots over the weathered
portions of the rock. Paler thin bands, very compact in texture,
occur in the southern part of the district: around Llangrannog.
The presence of crystals of iron-pyrites occasionally gives a marked
feature to the grits; and at Pen Craig, Llanilar, and in the Garthen
valley, Eglwys Fach, some beds occur beautifully studded with these
brassy cubes.
The ordinary thickness (4—6 inches) of the beds is very constant
throughout the area of the Aberstwyth grits; but more massive beds
(1-13 foot) occur under Allt wen and at Aberaeron, in the Garthen
valley, and at Llangwyryfon (24 feet). At Cefn Coch, Pen Pegwyns,
and along the coast south of Aberystwyth still thicker beds are seen
(3-4 feet); they are worked for building-stones. At the southern
limit of the series, near Llangrannog, the grits become thin, irreguler,
and inconstant, thus gradually dying away, to be replaced by the ar-
gillaceous slate-rocks. |
Two structural peculiarities are very characteristic of the Car-
diganshire grits—namely, the remarkable contorted lamination seen
on a fractured surface, and an abundance of fucoid markings, to-
- gether with strange-looking ripplings, ridgings, volutings, and other
raised forms of structure found upon the undersurfaces of the grit-
beds?. The rock is jointed, sometimes into large blocks good for
building- and flag-stones, but often much more closely into regular
oblong or rhomboidal fragments. At Allt-wen cliff and elsewhere
it is divided up into oblong, prismatic, or rudely lozenge-shaped
fragments a foot long, forming a kind of coarse grit-rab.
* This abundance of felspar crystals, so general in the Silurian rocks (Upper
Silurian of North Wales, South Wales, and the Lake-district), points to the
neighbouring presence of a vast mass of early, perhaps primeval, igneous
rocks as the great source of sediment-supply in Silurian times.
+ It is proposed to give a more particular account of the rock-structure of
Cardiganshire in a separate paper.
GEOLOGY OF CENTRAL WALES. 151
Little need be added to what we have said on the alternating
argillaceous beds. The rab-type is best seen upon tho Allt-wen
cliffs, south of Aberystwyth, where also au elongated type, serving
very well as rough pencils, forms the ‘“pencil-rab;” these beds
commonly appear much more solid in the heart of the rock, the
fragmentary structure only becoming developed after exposure to
weathering.
The cleavage phenomena here are often of peculiar interest from
their frequently incomplete, half-developed character. The dark shaly-
. looking rock of Constitution Hill, Aberystwyth, would not at first be
suspected of a slaty structure ; but Specimens may be gathered with
the cleavage seen distinctly cutting across the stripe- lines ; and many
of the dark, soft, shaly rock-beds of the neighbouring cliffs, when
seen in situ, will be found to have their shetsme) ies running
across the bedding.
A pale, homogeneous, hardened mud, or pale mudstone, splitting
with curved, conchoidal surfaces into 2-3-inch blocks, is of additional
importance, as probably marking a zone; I have found it some half
a mile north-east of Nant Kos, at Pen Craig, Llanilar, on the road-side
N.N.E. of Llanbardarn, and at five miles east of Aberaeron. This
appears to indicate a distinct zone near the top of the Aberystwyth
grits. The same kind of rock occurs at Llyn Fyrddyn Fawr, and at
Rhos Rhydd, near Llantrisant, where itis again not far removed
from the thin-flag series—another zone at the top of the Abery-
stwyth grits.
The Large-flag series.—This series, which belongs to the upper
part of the Aberystwyth group, is best marked to the east, in the
neighbourhood of the Devil’s Bridge and Llantrisant, where its
presence is soon made manifest in the construction of piggeries and
other low huts, whose sides and roofs are covered with the flags.
These are grit-beds, about 1 inch thick, but little jointed, so that
large slabs, frequently 4 and 6 feet square, are commonly extracted
for use in the neighbourhood. ‘The rock is fine-grained, and usually
exhibits a complete contortion in the lines of lamine; altogether
it much resembles some of the grit-beds of the middle Lingula-
flags of North Wales. The surfaces are gencrally undulated, and
often show true ripple-marks, over which we find Graptolites and
other fossils spread out: the Devil’s-Bridge Dendroid Graptolites
occur in this series.
The further extensions of these beds, north and south, are seen
around Pont Erwyd and south of Llantrisant; and the same series
seems to be brought up to day by folds, on the east at Hglwys -
Newydd, and to the west near the head of Cwm Symlog. Bands of
rottenstone (decomposed limestone) occur at the Devil’s Bridge, near
Eglwys Newydd, and again in the hills some four miles east of Tal
y bont.
Around Aberystwyth these flags are not so well developed; but
they may be recognized at Cefn Hendre, as already described, where
they are put to the usual purpose of hut-making for the work-
men’s shelter.
M 2
12 WALTER KEEPING ON THE
Fossil localities, other than those already given, are :—
Parson’s Bridge, and Temple Mine, south of Pont Erwyd.
Monograptus lobiferus, MM‘ Coy. Myrianites M‘Leayi, Murch.
Climacograpsus scalaris, His. Buthotrephis major, Keep.
Nereites Sedgwickii, Murch.
Cefn Coch, near Aberystwyth.
Monograptus Sedgewickiu, Pordd. | Retiofucus extensus, Keep.
Buthotrephis major, Keep. Paleochorda tardifureata, Keep.
minor, Keep. |
Constitution Hill, Aberystwyth; Wern Grug, Llanilar; Mynydd
Bach; Plas Crag, Llanbardarn, and other places have also yielded a
few fossils, mostly Alovw,—Buthotrephis major, B. minor, B. minimus,
Keep., Paleochorda tardifurcata, Retiofucus extensus, and Nema-
tolites Hdwardsu, Keep.
Thickness.—We have seen that much of the apparent thickness of
the Aberystwyth grits is deceptive, being explained away by great
folds. Still a great series remains, well attested even by the simple
heights of many hills which are built up entirely of this group.
Mynydd Bach appears to be over 1000 feet high (by aneroid); and
I should estimate the group at certainly not less than 1000 feet of
maximum thickness. Our detailed measurements along the Devil’s-
Bridge road show a thickness of 1639 yards, or nearly one mile.
The Metalliferous-slate Growp—A very large part of Cardi-
ganshire is constructed of this series. In the special area of our
work it forms a broad semicircular zone, some eight to ten miles
across, sweeping around the dome of the Aberystwyth grits to form
all the slaty country from north of Cardigan up to Machynlleth.
At the latter place it forks into two, the main curve being continued
out to sea by the Dovey valley, while a broad but rapidly attenu-
ating arm runs northward to Dinas Mowddwy, at which place its
much diminished representative is found between the Bala series
and the Tarannon shale.
The above area, however, is not unmixed metalliferous slate, the
upper part of the Aberystwyth group being brought up by folds,
along north-and-south lines, running through Ystrad Meurig, and
the Deyil’s Bridge; and possibly some outliers of the Plynlimmon
group may be folded in. Still the general absence of arenaceous
beds is marked over miles of country without a single grit-bed to
serve for road- or building-stone. ‘Tin Llidiart village uses the hard
pale slate of Goginan for building ; and at Llanafon the numerous
boulders serve for road-metal.
Further south, in the line between Cardigan and Llandovery, the
slate series appears in still greater extent, which is due to its there
representing also the Aberystwyth group, and perhaps also the
Plynlimmon grits, these groups not being developed as such in that
area.
A marked lithological character distinguishes this group as a
whole, the terms “‘ indurated shaly slate,” ‘irregular slate,” « flagey
slate,” ‘ pale blue slate,” from my note-book, serving to indicate the
usual character; I also find “hard pale slate-rock, often much
GEOLOGY OF CENTRAL WALES. 158
jointed,” and “pale slates with ribbon bandings.” ‘The prevailing
colour of the rocks is a pale blue-grey ; and they generally break up
into moderately small fragments, shale-fashion.
Slate.—In many places where the slates are better cleaved, and
less frequently jointed, they are worked in small quarries for inferior
local purposes, as around Llancynfelin, in the hills south of Machyn-
lleth, in the island mounds of the Gorsfochno flats, and near the
Devil's Bridge. These rough slates are pale-coloured, hard, and
coarse; but around Machynlleth thoroughly good slates are worked
in anumber of large quarries. One of the largest of these is at Pont
Faen, where large slate-flags are extracted ; but the most interesting
to the geologist is that at Morben, two and a half miles south-west
of the town of Machynlleth. These are thick-hedded slate rocks,
with a few thin grits, dipping at high angles to the W.N.W.
This, however, is an inverted dip, a8 is proved by the position of
the prominences on the grit-bands, which are upon the upper sur-
faces of the grits, the worm-trails being also manifestly in inverted
position. ‘The cleavage-dip diverges only slightly from the bedding-.
dip, so that the Graptolites usually run for some distance along the
surface of the slate, and then gradually skim under it. The slates
are very good, dark and soft. Nodules of iron-pyrites occur; and
nearly all the Graptolites are converted into this bright mineral.
This quarry has yielded the finest of our fossils, the Monograptus
Sedgewicki being especially magnificent.
Fossils from Morben Quarry, Machynlleth.
Rastrites peregrinus, Barr. Monograptus Hisingeri, Carr.
maximus, Carr. -—— tenuis, Portl.
Monograptus Sedgewickii, Pord/. myolutus, Lapw.
— , var. spinigerus, Wich. Diplograpsus Hughesu, Nich.
—. , var. distans, Pordd. Climacograpsus normalis, Lapw. ?
—— intermedius, Carr. Myrianites M‘Leayi, Murch. ?
spiralis, Geinitz. Lapworthii, Keep.
——- lobiferus, M‘Coy. Buthotrephis major, Keep.
Below this in present position, but by inversion really above it, is
a zone of pale blue and olive shaly slate, pointed out to me by
Mr. J. EK. Marr, F.G.S., as being similar to certain zones in the
Coniston mudstones. The great slate district of Corris, usually
referred to the Llandeilo age, is in this series, as will be shown
later on; also the excellent slates of Dol y Mynach and Cwm par
Adwys, west of Rhyader.
Other rock-varieties, such as dark paper-shales, rab, and mud-
stone, approach near to the Aberystwyth types; and some of the
occurrences of such rocks doubtless indicate the uprising of that group
as inliers in the metalliferous-slate area. In the Devil’s-Bridge
road such rocks appear in several places.
Grit-beds as thick as 6 inches may occur; and thin zones, about
4 inch to 2 inches thick, are frequent; these are generally red-
stained at the surface, and micaceous. ‘They are trustworthy guides
to the dip of the beds, which in their absence is often not easy to
discover.
154. WALTER KEEPING ON THE
At Cwm Symlog, nine miles east of Aberystwyth, pale soft shales.
and slates with thin grits, rich in fossils, are found.
Fossils from Cwm Symlog.
Rastrites peregrinus, Barr. Monograptus palmeus, Barr.
Monograptus Sedgewickii, Port. Climacograpsus spiralis, His.
crenularis, Lapw.
FORAMINIFERA.
cog ee ape _Dentalina.
eregarius, Lapw. :
intermedius, Carr. Textularia.
—— Clingani, Carr. Rotalia.
spiralis, Gezn. ANNELIDA.
lobiferus, M*Coy. Nereites Sedgwickii, Murch.
runcinatus, Lap. Myrianites M‘leayi, Murch.
—— Hisingeri, Carr. , Nemertites Olivantii, Murch.
tenuis, Portl.?
involutus, Lapw. ALG.
Diplograpsus tamariscus, Nich. ? Buthotrephis major, Keep.
Hughesii, Nich. minor, Keep.
sinuatus, Nich. —— minimus, Keep.
At Ystrad Meurig, forming the high ground twelve miles south-
east of Aberystwyth, and in near association with a fossil zone, is a
series of hard pale grits with thin indurated slate partings, firmly
bound together, to form hard massive rocks (a); we refer to this as
the “Strata Florida rock.”
Another well-marked rock demanding attention is (6) a pale indu-
rated slate rock, usually cross-banded by thin arenaceous stripe-
zones. It is well seen at Machynlleth, to the east of Kglwys Fach,
and east of Tal y bont. Again, the same type of rock occurs (c) in
the hills east of the Rheidol gorge; I find blocks of it around Llan-
trisant; and it is also well developed at Goginan, to the east of
Llanddewi Brefi, and in the hills west of Rhyader. These rocks
are essentially similar to those of Ystrad Meurig, only less arena-
ceous; and I include them all under the name of “Strata Florida
rock.”
Now, classifying these various localities of the Strata Florida rock,
we find they fall into a set of definite lines having similar relations
to neighbouring rock-beds, and indicating, as I believe, definite
zones. First, the more arenaceous rock of Ystrad Meurig is in the
same north-and-south line with Cwm Symlog and with Llantrisant ;
and in the first two of these places it is in near relation with a rich
fossil zone. Also it is about in the same line with the Large-flag
series, as seen in the Devil’s-Bridge road, nine miles east of Aberyst-
wyth, also found at Llantrisant aud Cwm Symlog. In these places
we have, then, evidence of the occurrence of this hard pale slate rock
along a definite line of country in near association with the Grap-
tolite fossil-zone and the Large-flag series. Next we find that the
group b also falls into a line east of Aberystwyth; and here, again,
it is associated with the great fossil zone at Machynlleth, while near
Tal y bont it is connected with a band of rottenstone like that of
the Large-flag series at the Devil’s Bridge.
Altogether, then, the result of these lithological correlational is to
support our theory of four different lines of north-and-south foldings
GEOLOGY OF CENTRAL WALES. BUS,
between Aberystwyth and Plynlimmon—namely, (1) the principal
axis of Aberystwyth, (2) the principal axis of Plynlimmon, and (3)
the two minor axes running (a) from Ystrad Meurig through Llan-
trisant and Cwm Symlog, ‘and (5) along the gorge of the Rheidol
about Pont Erwyd and the Devil’s Bridge. The further northward
extension of (a) is probably indicated by the grits of Yr Carreg and
Moel y Llyn. These minor folds have not been recognized further
south ; and, indeed, we might expect them to disappear as the lateral
spread of the beds becomes restricted.
At Lampeter the well-known olive shales and grits with Werettes
&c. are exposed in quarries. The grits are in thin beds (2-4 inches),
hard and laminated, with partings of shale either light (olive) or
dark in colour; no cleavage is seen. The fossils are :—
Nereites Sedgwickii, Murch. Nemertites Olivantii, Murch.
-— cambrensis, Murch. Palzochorda tardifurcata, Keep.
Myrianites M‘Leayi, Murch. Retiofucus extensus, Keep.
also other worm-like and algoid markings. -Altogether this is a
pretty typical metalliferous slate, though more arenaceous than is
common,
Fig. 3.—Railway-cutiing between Traws Coed and Caradoc
Waterfall, 1877.
Contortions.—The woodcut (fig. 3), representing a railway-cutting
east of Traws Coed, illustrates some of the frequent and sharp contor-
tions of this series. All the perceptible foldings, however, numerous
and striking as they are, are far from adequately showing the real
complexity of the infinite twistings and inversions of this series, the
existence of which is proved principally by considerations from the
fossil evidences. Without fossil evidences it is, as a rule, impossible
to detect inversions; but still, in those places where grits with
fucoidal markings &c. occur, we have another key to the true rela-
tions of the rocks—namely, in observing the positions of the curious
prominences upon the surface of the grit, these being normally
always upon the under surfaces; but where the beds are inverted
(as at Morben, Machynlleth, &c.) they are found upon the upper sur-
faces, the true worm-trails (Nereites &c. ) being in this case Sapresed
upon the under surfaces, in inverted position.
These inversions explain away in great degree the enormous
apparent thickness (miles of strata) of this series; but a very great
vertical series still remains well attested in actual steep and preci-
156 WALTER KEEPING ON THE
pitous mountain-sides, from 500-1000 feet high, and I cannot esti-
mate the group at less than 2000 feet.
Fossils are almost entirely wanting in this series, except, I be- -
lieve, near the base, where I would place the rich beds of the
Morben Quarry, Machynlleth, and Cwm Symlog. The fauna is
intimately related to that of the Aberystwyth group, as indeed was
to be expectec ; for the fossils of this latter group occur in its higher
part, not far removed, in serial order, from the Metalliferous-slate
fossil-zone.
The worm-like and fucoidal markings, Nereites, the Fan Algal,
and the Nematolites are widely distributed throughout the series,
worm-trails being very characteristic.
Other fossil localities are :—
Llantrisant, with the large Fan Algal (Buthotrephis major) and
Nematolites tubularis, Keep.; the Llyfnant valley, with Climaco-
grapsus scalaris, His. ; Dyffryn Castell, with Climacograpsus scalaris,
worm-tubes, and the Nematolites, also some of the shells recorded
by Sedgwick ; and Steddfa Gurig (west of), with Monograptus Sedge-
wickri, “Portl., M. tenuis, Port. ?, Climacograpsus scalaris, His., and
Orthoceras. ‘Above Taliesin, frasments of dendroid Graptolites and
Nemutolites tubularis occur ; sm the latter is also found at Llantri-
sant, Ty Llwydd, on the Rheidol, and elsewhere.
Richer localities are :—
West of Lisburne Mine, Ystwyth Valley.
Climacograpsus scalaris, His.
Nereites Sedgwickii, Murch.
Buthotrephis,
Rastrites ?
Monograptus Sedgewickii, Pordl.
spiralis, Gein.
-—— lobiferus, MM‘ Coy,
Garthen Valley, Melin Newydd.
Monograptus Sedgewickii, Por?/, Orthoceras, sp.
Climacograpsus scalaris, Hs.
The numerous metalliferous veins (lead and silver) in the rich
mining-districts of Cardiganshire are almost confined to this set of
beds; hence the name here given it.
3. The Plynlimmon Group.—As we ascend the mountain-slopes
along the valley of the Rheidol, above Pont Erwyd, we meet with
the rocks of the upper grit series, which form the upper part of the
Plynlimmon mountain. Around Garn Fach some of the grit-beds
are seen, of rather coarse type, sometimes assuming a very grani-
toid aspect, there being a profusion of felspar crystals and large
blebby quartz grains. The felspar crystals may be of large size; and
some of them are perfectly preserved and glassy. Doubtless the
rock is the direct result of the degradation of an ancient acidic
igneous rock.
Conglomerate beds, consisting of pebbles of white quartzite and
vein quartz in a grit matrix, are also met with; but they are few.
The group here is still, in the main, a slate series, some of the slate
being pale and papery, of the “ pale-slate type.’ Iron pyrites is
GEOLOGY OF CENTRAL WALES. 157
common in both grits and slates. The main dip is decidedly
easterly.
Mounting the higher ground above Nant y Moch the grits become
more conspicuous, forming a terraced structure by their outcrops
around the hill; and near the summit a rugged steplike structure is
produced by the regularly bedded fine-grained grit series. The
finest exposure of these Plynlimmon grits is in the magnificent pre-
cipices fronting the Rheidol lake (Llyn Llygad Rheidol), where
many of the beds are very thick (7-10 feet) and of moderately
coarse grain. A particular feature in them is their regular columnar
jointing; this is quite as regular as in many columnar felsites,
numerous columns, 7 feet long, being seen running right across the
beds. Conglomerates are uncommon; but some three or four beds
of beautiful “pudding stone,” with white quartz pebbles in a fel-
spathic sandstone matrix, are seen upon the western slope of the
mountain.
Coarser beds of this group are probably indicated by a large
boulder upon the hill-top above Gogerddan House, near Aberystwyth,
which has pebbles as big as cannon-balls.
These grits form a crescent zone from north of Plynlimmon
through the high ground of Mid Wales, running east of Tregaron
and east of Lampeter; but they die out beyond this to the south.
They constitute the genuine backbone of South Wales, lying in a
synclinal. The highest beds form the upper ground of Plynlimmon
itself. In the Teifi area the beds are remarkable for being coarsely
eleayed into large tiles about 4 inch to 1 inch thick, a structure
which graduates into jointing on the one hand and true slaty
cleavage on the other. Similar cleaved grits occur around Llyn
Fyrddyn and on the hills east of Lampeter, all of which I would
place on the same horizon. There is, however, some doubt in my
mind as to the exact position of this horizon in the geological
series.
Foldings.—As a group, the Plynlimmon grits are characterized,
not by violent contortions or sharp bendings with fracture, but by
broad and gentle foldings. These are beautifully seen around the
Teifi lakelets and Llynodd Ieuan; also at Llyn Fyrddyn Fach and
Llyn Fyrddyn Fawr, and Llyn Bugeilyn, where the ridges and minor |
hog-backs of the surface correspond with the structural anticlinal
and periclinal foldings of the rocks with great regularity and
clearness.
Amongst the rock-varieties we may notice blue shaly slates, blue
slates in 6-inch beds, cleaved into oblong flags about 3 inch thick
(Llynodd Ieuan), and arenaceous mudstone, broken up into coarse
rab, the fragments measuring 1-3 feetx3 inchesx1 inch, also
smaller rab.
The lithological differences between this series and the Aberyst-
wyth group are the greater thickness of the grit beds, the presence
of quartz conglomerates, and the rarity of curious rock-surfaces and
fucoidal markings. The slates also are, as a whole, of paler type.
Fossils have not been discovered in the grit series of the Plyn-
158 WALTER KEEPING ON THE
limmon mountain; but large boulders of coarse conglomerate upon
Gogerddan Hill, Aberystwyth, which surely came originally from
this mountain, contain casts of various fossils, of which I can men-
tion crinoid ossicles, Nebulipora?, Petraia, a large cup coral, and
Meristella.
The thickness of this group must also be very great; for Plyn-
limmon rises some 1500 feet above Garn Fach, the level where the
Plynlimmon grits first appear. A thousand feet is probably an
under-estimate.
Part Il. Brief Notes upon other Sections.
(1) From Aberystwyth through Pont Erwyd to near Builth (fig. 4),—
From Aberstwyth to Pont Erwyd the section is similar to that from
Aberystwyth to the Devil’s Bridge; but the western dips are more
important towards Pont Erwyd, so that the inversions required are
here smaller or less numerous. Beyond Pont Erwyd is a great slate
and shale series running for many miles, nearly to Rhyader, and
forming by the apparent dips an important synclinal under the highest
ground south of Plynlimmon. Fossils occur at Pont Erwyd and
Dyffryn Castell, also near Rhyader. The hard pale-slate series comes
in at Goginan and east of Pont Erwyd, and there is a similar rock
west of Rhyader; but the Plynlimmon grits do not actually appear
as such, unless the grits of Llynodd Ieuan belong here; they are,
however, well developed in the mass of Plynlimmon further north.
Some of the paler slate along our line of section may represent this
series. Grit beds similar to those of the Aberystwyth group are
found in two places near the ‘Glansevern Arms,’ and again further
on east of Langwrig. ‘They are to be regarded as special local de-
velopments inthe Metalliferous Slates. Other grits and conglomerates
seen at Gwastaden are probably the representatives of the Plyn-
lmmon grits.
(2) Section from Llandeilo to Aberaeron.—Three principal grit-
areas are met with in the line of this section—namely, at Talieris
(west of Landeilo), east of Lampeter, and at Aberaeron. The Talieris
conglomerate beds are surmounted by dark shales and shaly slates
of the Metalliferous types ; and beds of the Rhyader pale-slate type
next underlie the grits of the country east of Lampeter. By an
exceptional appearance the Metalliferous slates of the west seem to
underlie the Aberaeron grits. No pale slates are seen beneath the ~
Talieris conglomerate beds. The principal axial fold in the section
seems to be a synclinal in the Teifi valley by Lampeter—the
mountains to the east and west of this being (that is, if the rock-
dips have any truth in them) great anticlinals in the Metalliferous-
slate and Rhyader Pale-slate series. The beds of grit and con-
glomerate at Talieris are not of the nature of basement beds of a
stratigraphical group, but indicate nothing more than such slight
physical variations as a shallowing of the sea-bed or a change in the
direction of the currents, resulting in the formation of sand and
pebble banks ; for the pebbles are not fragments of the underlying
rocks, and there is no trace of any physical break or even change of
lithological character above and below them.
159
GEOLOGY OF CENTRAL WALES,
"SOJEIS OV "PF ‘oyvys ATOATYS pure ‘ssvy pur sqias uy, *z
“SOIVIOTLO[SMOD PUL SII *G “SOTVYS PUL SeqVIS B[eq “ ‘goye[S pu ‘soreys ‘s}las yaeq *T
¢ F | g I
, i NON esses 20/20 Sa S
J 4, RENE Ze : Ss oe bn 5
ce
Q “ropedyy ‘jeyon | “UCT WMO ‘qo1o £ went gE *Lapeg Jury "TIeT, WOAIOeO "B[00g FOE
Bao Sopvyueyy f
Patel fee
. S m
"a e “M
Copu 8 07 TOUT + “oTVos TeyUOZTIOF,)
“uapmisvmy pun sapohyar 07 spoog afiaT 22 pun nprwopst VID) Wouf W0LNDI2gG—'G *SIyT
‘jeurpouds tomutpudTg °9 "SOIVIOULO[SUDD) “F "A1ZUNOD P219A00-JJIICL *Z
¢ SUOISIOAUT “9 "SOJLS OMT ‘ “S}IAG UIY} MOF V YIM ‘SOTLOS O}VIS-SNOIOFIT[VIONL *T
SS
Soxt
AD
D
SN
{
J
!
I
1
‘
!
1
t
i
x "Stamp VF pperg
= Sos nfs
Topryseay ‘ropesyyy -SramBavyy *[00
*ppAMAFT 40
“O'S$<—ax PpAMIT FUOg
m—>"M'N ‘<—as ep—>" M
‘wapoliyy puw biumbunyy 07 svn vomunuliyg oyn ybnouy phnag wwog wort wy0y—'F “Stir
160 WALTER KEEPING ON THE
(3) Rhyader to the Teift Pools
(fig. 5)—In this section three
main folds are indicated, namely a
central anticlinal fold at Disgwylfa
in the Rhyader pale slates, with a
synclinal on its east and west.
The former is a comparatively
simple basin of pale slates beneath
the grits and conglomerates of
Cwm Elan and Gwastaden; the
latter, corresponding with the
Plynlimmon synclinal, is a much
more complicated structure, pro-
bably much affected by reversals.
General Result of the Hast and
West Traverses (see fig. 6).—The
sections just indicated show that
the great area of Mid Wales is
made up of a thick series of im-
perfect slates, pale slates, shales
and grits, having a general re-.
semblance and intimate connexion
throughout, as of one continuous
group, but divisible into the sub-
groups indicated in the beginning
of this paper.
These rocks form one great pri-
mary synclinal extending from the
Aberystwyth axis to the east of
Rhyader, and from the west of
Llandeilo to Aberaeron. For in
the west of Cardiganshire we find
a great and continuous course of
easterly dips running inwards from
the coast; and in the eastern half
of the area, in Radnorshire and
Caermarthenshire, is a correspond-
ing grand set of westerly dips.
Subordinate but still very great
anticlinal folds along north and
south axes bring up on the east
tee Metalliferous slates between
Plynlimmon and Rhyader, and on
the west the upper part of the
Aberystwyth grits, in the line of
Pont Erwyd and the Devil’s
Bridge. Another, smaller fold
with the same result as the last,
runs from Ystrad Meurig north-
wards towards Machynlleth, thus
Rhyader.
3. Rhyader pale slates.
f. Plynlimmon grits
Plynlimmon.
rous-slate group.
Fig. 6.—Diagram of the General Structure of Central Wales.
yth grits.
1. Aberystw
Metallife
2.
Aberystwyth.
{
GEOLOGY OF CENTRAL WALES, 161
greatly swelling out the surface-area of the Metalliferous-slate
series.
~ Minor foldings, also with north-and-south axes are infinitely
abundant over the whole district, with frequent inversions which
obscure the original order of the rock-beds.
Included in these foldings are four principal crescent zones of
grit, greywacke, and conglomerate, namely :—1Ist, the western or
Aberystwyth grits; 2nd, the eastern grits—an imperfect line of
grits seen at Talieris, west of Llandeilo, and perhaps continued in
other grits Kast of Gwastaden. These I regard as the diminutive
representatives of the Aberystwyth grits. 3rd. The Plynlimmon
grits and conglomerates, with much associated pale slate; and
Ath, the grits and conglomerates of Cwm Elan and Gwastaden, which
are also associated with, and, indeed, included in, a great pale-slate
group, the Rhyader pale slates. The last two are upon the same
stratigraphical parallel, occupying synclinals. These grits I do not
regard as necessarily holding exactly the same horizon over wide
areas, they having been probably shingle banks over the old
sea-bottom. The pale slates seen in so many sections appear
to belong to two principal horizons—(a) the lower or Strata Florida
pale slates in the lower part of the Metalliferous-slate group, and
(6) the Rhyader pale slates, associated with the Cwm Elen, Gwastaden,
and Plynlimmon grits.
More distant Sections (see Table of Vertical Sections, p. 164).
In order to work out the relations of these rocks to the other
lower paleeozoic groups, I have visited various districts where the
Cardiganshire series might be studied in association with rocks of
some definite and decided horizon—namely, amongst other places,
Llanbrynmaer, Dinas Mowddwy, Cardigan, N. Wales, &c.
In the Llanbrynmaer area we find (1) an upper series of grey
grit and greywacke, often very felspathic and micaceous, cleaved,
and with fragments of fossils (the Denbighshire grits). These pass
down by gradual transition into (2) a series of pale blue and green,
grey and purple shales, with some darker shale, rab, and green grits,
which make up the true Tarannon shales; some obscure fragments
of Graptolites have been found here. Again, there is no break, but
a simple passage between this series and (3) the lower series of
grits, greywacke, and dark shales which belong to the Cardiganshire
type, and contain the fossils of our Metalliferous group. To the
west of the Tarannon plateau we find the Metalliferous slates fully
developed in the Pennant valley, with the characteristic fossil species,
and the usual associated lead-mines of that group.
The whole character of this Metalliferous slate is different from
that of the Tarannon shale; and our evidence points uniformly and
decisively to the Metalliferous slate being a more ancient series, the
two groups being separated in this area by a zone of grits. The
Plynlimmon grits and associated pale slates, as seen in Plynlimmon
and around Rhyader, appear to be wanting in this area, there being
no well-developed grit series between the Llandovery group and the
162 WALTER KEEPING ON THE
Denbighshire grits. We shall find reason to believe that they are.
represented, feebly it is true, by the thin grit-beds above described
in the Tarannon shale.
The Dovey Valley : Section across the valley near Llany Mowddwy
(fig. 7)—This section gives, in a narrow area (measuring less
than 2 miles across), the complete series from the Lower Bala slates
tothe Denbighshire grits. The Denbighshire grits pass down into
the Tarannon shales, which are pale-slate rocks resembling the
Rhyader pale slates. There is, again, no break between these and
the series of greywackes and dark shales and slates beneath. ‘This
latter group (which is in part the Lower Llandovery of the Survey)
agrees both in its lithological characters and in its fossils, so far as
known, with the Aberystwyth grits.
There is no distinct basement bed of conglomerate or grit to this
series, such as might indicate the existence of an important strati-
graphical break ; but, on the contrary, there is every appearance of
a passage from the underlying great slate group up into the true
Silurian series. This great slate group corresponds in its general
lithoisgical characters and its “ cone-in-cone” nodules with our
Metalliferous slates; but I have not detected any pale slate in them.
In the absence of fossils, it is not possible to determine their exact
age; but they should probably be regarded as belonging for the most
part to the Upper Bala slate group. I should, however, expect
some of its upper beds to be the representatives of our Cardiganshire
Group, the lower part (Upper Bala) corresponding with much of the
slate group between Cardigan and Llangrannog, about to be de-
scribed.
It is further noteworthy that im this line of section, as in the
Cardiganshire Group, the newer rocks are much better cleaved, and
appear altogether more highly metamorphosed than the more ancient
rocks to the west.
Corris Avca.—The great slate district of Corris, usually referred
to the Llandeilo age, belongs to our Metalliferous-slate group, as is
proved by the following fossils from Corris and Taren y Gesail :—
Monograptus Sedgewickii, Portl.? Climacograpsus scalaris, His,
—- tenuis, Portl.? Orthoceras, sp. (same as the Cefn-
Hendre shell).
The Cardigan District.—The pale felspathic grits and black slates
of Newport Bay and Cardigan, hitherto placed in the Lower Llan-
dovery series “‘b 4,” are not of this age, but belong to the Middle Bala
or Caradoc Group ; as to this the fossil evidence is conclusive. Above
these come rolling beds of pale slates and shales, then darker shaly
slates, with a zone of pale felspathic grits; these also I refer to
the Bala period. The overlying shaly slates and rab are passage-
beds of Caradoc-Llandovery age, presenting the gradual incoming
of the Aberystwyth grits.
Reviewing the several rock-groups and their distribution, we find:—
(A) The Plynlimmon grits, seen upon Plynlimmon and around
Rhyader, also probably in the hills west of Tregaron and Lampeter ;
163
GEOLOGY OF CENTRAL WALES.
Dark slates (Lower Bala).
Bala ash-bed.
Bala limestone. -
Bala phosphate-bed.
Calcareous slates and flagey
shales.
ig. 7.—Section through the Dovey Valley at Llan y Mowddwy.
(Horizontal scale, about 23 inches to the mile.)
Lian y Mowddwy. Cwm Maenydd. Waterfall.
6. Imperfect slates, dark shaly and 9. Hard pale slates, banded slates, well
rubbly slates and shales. cleaved (‘Tarannon group).
7. Dark-coloured irregular slates, with 10. Dark rab and coarse gritty rab, and
“‘eone-in-cone” nodules. grit bands (Passage-beds).
8. Grits, dark shaly slates, and rab. 11. Denbighshire grits, with dark rab
Fossils (Lower Llandovery). and slates.
164 | WALTER KEEPING ON THE
but they die out to the north and south of these localities. No
fossils have yet been detected in this series in Cardiganshire, except,
perhaps, in the boulder-block at Gogerddan, near Aberystwyth.
Stratigraphically they lie above the Metalliferous slates; and these
latter are proved, in the Llanbrynmaer, Dovey, and other areas, to
be inferior to the Tarannon shales. Therefore, with reference to the
Noedd Grug section, they must either represent the uppermost part
of the Llandovery rocks or a special gritty development in the Taran-
non shales. I adopt the latter view for the following reasons :—
because of (1) their dissimilarity to the grits (Llandovery grits)
which underlie the Tarannon shales at Llanbrynmaer, Llan y
Mowddwy, and elsewhere ; (2) their association with pale slate rocks
similar to the Tarannon shales of the Corwen area; and (3) the oc-
currence of such a group of rocks, the Gala grits*, in this position
in the south of Scotland. Moreover, in the Tarannon district the
first appearance of such a development of grits in the Tarannon
shale is already seen in the numerous thin grits, with contorted
structure, of Tarannon Hill, Llanbrynmaer. The Rhyader pale
slates thus appear also to belong to the true pale slate or Tarannon-
shale series.
(B) The Metalliferous slates, which are enormously developed,
spreading over a very wide area of Mid Wales. ‘They maintain one
general lithological character of hard, pale, shaly slates, also containing
a zone of pale slates. The group is generally plumbiferous.
(C) The Aberystwyth grits may be taken as an arenaceous de-
velopment of the Metalliferous slates, in its lower part. Like the
Plynlimmon grits they die out to the north and south, their southerly
attenuation being well exhibited around Llangrannog. They dip
persistently under the Metalliferous slates ; and the truth of this dip
is proved by the position of the contorted raised structures upon the
under surfaces of the gritst.
In the Dovey valley the Aberystwyth Grits are represented by
eritty beds of a similar character; but here they appear to belong
to a slightly different horizon, namely to the upper part of the
Metalliferous slates; and the same is true of the grits exposed in
the deep Talerddig cutting, Llanbrynmaer. The grits and conglome-
rates of Talieris, west of Llandeilo, very probably belong to the
horizon of the Aberystwyth beds. In the Noedd-Grug section these
beds, together with the Metalliferous slate, are represented by the
Llandovery group of the Geological Survey, probably the Upper and
part of the Lower Llandovery ; but from the fossil evidence we can-
not recognize the lowest part of the Llandovery Group (Lower Birk-
hill) in Central or West Cardiganshire. Part of the lower set of
slates beneath the grits, described in the Cardigan and Dovey areas,
* Mr. Lapworth, F.G.S., writes me that “all the paleontological affinities
of the Gala beds are with the Tarannon shales, with which, and not with the
Upper Birkhill beds, they must eventually be connected.”
+ Ihave confirmed this test by examining the beds of Lingula-flags, Trema-
doc and Bala rocks of South Wales, where these curious worm-like, fucoidal,
and irregular prominences are found uniformly upon the wader surfaces of the
grits.
les and othe
6. Abery,
and Plyn
Pale |.
Shales, | ~~
Mudstone
Group.
Bala
Group. ||
a
ae
a we
wit.
ore
Fr
2 South Scotland
(Lspworth).
3. South-west
Cardiganshire.
Comparative Vertical Sections of Silurian Rocks in Central Wales and other Localities.
5. West of
Llandeilo,
6. Aborystwyth
4, Rhyader,
Plynlimmon |
Grits. |
Grits.
alee peers
Pale Slates.
Metalliferous
Slates.
MUM
WOME
CMM
TT)
WMUMLLA
Aberystwyth [=
Gnits.
ee
MM PTL
LYM
| HMMM
WW
and Plynlimmon.
7. Lianbrynmaer,
Denbighshire
Grits.
Tarannon
Shales. (AF
LZ
V7
8, Llan y Mowddwy,
|
ie
Bala -
Limestone.
[Vo fuce puge 164,
9, Clwydd Valley
(Prof, Hughes).
Corwen ===
Grits. |
GEOLOGY OF CENTRAL WALES. 165
probably belong here and complete the series ; for we have seen there
is no break of continuity down into the Bala formation.
Part III. Paleontological Evidence.
Although the order of succession of the forms of life have in all
eases been first determined from the results of stratigraphical re-
search, yet, that order once established, the organic remains, as
considered in groups, become the supreme test of the age and rela-
tive order of rock-masses—superseding, and in some cases actually
overthrowing, the apparent evidence of succession in the rock-beds.
Such we find to be the case over a large area of Cardiganshire,
where, as in the section from Aberystwyth to the Devil’s Bridge, the
stratigraphical series, seeming to be continuously ascending through
some three or four miles of thickness to higher and higher beds,
is proved by a handful of Graptolites to be radically misleading ;
for, the fossils being identical at almost the extreme ends of the
section, the true reading is shown to be a series of inversions, by
which the original order of the beds is obscured. Thus, over a large
part of Mid Wales, it is to the organic remains alone that we can
look with confidence for unravelling the apparently inextricable, and
often delusive, tanglement of the strata, and establishing their true
succession.
The most important element in our paleontological evidence is
the group of Graptolites, these fossils having now become, through
the most successful work of Mr. C. Lapworth, F.G.S., of the highest
value in Cambrian and Silurian geology. All my work in this
branch of study is based upon the published results of that geologist :
and I am also particularly indebted to him for examining many of
my Graptolites, as indicated in the Table (p. 170), and for valu-
able notes upon them conveyed to me in letters, from which I have
quoted below.
A study of the Table brings out a number of important facts.
At the first glance it is clear that all our fossil lists exhibit
one and the same general geological fauna. Our richest localities
are Cwm Symlog (eight or nine miles east of Aberystwyth) and
Morben (near Machynlleth), also Cefn Hendre, Cwm, and Bryn y
Carnauin the neighbourhood of Aberystwyth). A single one of these
localities (Cwm Symlog) yields every species, except four, of the
true Graptolites known in Cardiganshire ; and this, together with
the intimately allied fauna of Morben Quarry, includes all our spe-
cies except one (Monograptus turriculatus).
The other forms of life show no less clearly the unity of our
fossiliferous Cardiganshire rocks. The Orthoceras is wide-spread
in the Metalliferous Slates, and occurs also amidst the Greywacke-
Flags of Cefn Hendre; and the various forms of Alge and worm-
trails are also characteristic of the whole range of the Cardiganshire
group.
For the typical area of reference for Graptolitic deposits we must
unquestionably look to the rich beds in the south of Scotland, of
Llandeilo to Wenlock age, which have been so thoroughly worked
Q. J.G.S. No. 146. N
166 WALTER KEEPING ON THE
out by Mr. Lapworth. And here the reading is decisive: our Cardi-
ganshire series belongs not to the Glenkiln (Llandeilo) or the Hartfell
(Bala) periods, when the Didymograpti and Diplograpti flourished, but
to that part of the newer or Silurian era when the Monograptide
were predominant, and in their greatest development, namely the
Llandovery period (Birkhill Shales).
The more detailed affinities of our fauna will appear by a study
of the last five columns of the ‘‘ Table of Distribution.” Every one
of our species of true Graptolitide (excluding the Cladophora) occurs
in the Upper Birkhill beds of Scotland. Eight species are common
to the Lower Birkhill Shales, and nine (as also two species of Cla-
dophora) to the overlying Gala and Tarannon groups.
Of the fossils of the two principal Graptolitic localities, Cwm
Symlog and Morben, Mr. Lapworth writes that they ‘‘lie within the
same general Graptolitic zone.” .. . “‘ Of the nine species recognized
in the slates of Morben, five (namely Rastrites maximus, Carr.,
Monograpius spinigerus, Nich., MW. distans, Portl., M. Hisingere,
Carr., and Diplograpsus Hughesiz, Nich.) make their first appearance
in the Upper Birkhill Shales of 8. Scotland. astrites maximus is
confined to the highest zone of that formation, in the Moffat area,
and, together with its common associate, Dipl. Hughesii, seems to
have become extinct before the deposition of the overlying beds of
the Gala group.
“¢ The second fossil locality (Cwm Symlog) is even more strikingly
marked by its Upper Birkhill Graptolites. Sixteen forms have been
identified from this spot. Of these, seven species (viz. Monograptus
crenularis, Lapw., MV. pir Ge Carr., M. Clingani, Carr., MW.
runcinatus, Lapw., M@. Hisingeri, Carr., Dipl. Hughes, Nich., and
D. sinuatus, Nich.) are forms which are known for the first time in
the Upper Birkhill of S. Scotland, and its equivalents in Girvan,
Treland, and the north of England. J. intermedius, M. runcinatus,
and M. crenularis are peculiar to the Upper Birkhill, as also is M1.
Clingani, which is confined to a small seam in the very centre of the
Birkhill beds.”
Of the nine species of true Graptolites common to our Mid-Wales
rocks and the Gala and Tarannon, not one is a special Tarannon
form. Monograptus turriculatus, however, is most frequent in those
beds; and the two species of Cladophora Dictyonema venustum,
Lapw., and Rhizograptus ramosus, Lapw., are only known, else-
where, in the Gala group (Scotland).
From the fossil evidence, therefore, there can be no hesitation in
referring our Mid-Wales rocks to the same age as the Upper Birk-
hill of Scotland; and beyond the occurrence of the three species
just mentioned in the rocks of the Devil’s Bridge, there is nothing
that conveys the slightest hint that any of our strata are newer than
Upper Birkhill.
Lake District.—Fifteen of the Mid-Wales Graptolites are known
from the Coniston or Graptolitie Mudstones of the Lake District; so
that, in Mr. Lapworth’s ,words, ‘‘ the general facies of this Mid-
Wales fauna is distinctly that of the Coniston Mudstones.” These
GEOLOGY OF CENTRAL WALES. 167
species are nearly equally distributed in the two zones (tenwis- and
argenteus-zones) of that area. Also, amongst the other fossils, Mr.
Marr recognizes the fragment (tail) of a Phacops, found by him at
the Devil’s Bridge, as a new species also occurring in the “ Mud-
stones” of the Lake District.
Lithologically we find some of the Graptolite-bearing beds not
unlike part of the Coniston Mudstone series; and some paler
shales and slates, associated with the Graptolite beds at Morben,
Machynlleth, and occurring again at Cwm Symlog, have their repre-
sentatives also in the same series. Still, regarding them as a whole,
our Cardiganshire rocks decidedly do not resemble their representa-
tives in the English lake country.
We have seen that our verious fossil lists indicate that all the
fossiliferous beds belong to one general horizon. Certain minor
differences, however, are to be observed, of which the most important
are the presence of Monograptus turriculatus at Cefn Hendre and the
Devil’s Bridge, and the species of Cladograpt: of the latter place,
which are common to the Gala group of Scotland.
From the Graptolitic evidence Mr. Lapworth would arrange the
beds in the following order :—
D. The M. turriculatus beds of the Devil’s Bridge.
C. Next below (or perhaps identical with (D)) the Cefn Hendre
erits.
B. Then comes the rich Graptolitic zone of Morben and Cwm
Symlog.
A. Lowest of all lie jointly the Diplograpsus beds of Taren y
Gesail, Corris, and Steddfa Gurig.
It will, however, be seen that this order does not correspond with
our well-established succession of the greater groups as given in
the first pages of this :paper; for it would make our Metalliferous
slates newer than the Aberystwyth grits. Now, with all my general
confidence in fossil evidence, | consider that the paleontological data
are here insufficient to maintain this order against the very strong
stratigraphical evidence to the contrary., The principal fact is the
occurrence of a single species (Monograptus turriculatus) in certain
localities ; and this does occur, only less commonly, in the Birkhill ©
shales as well as the Gala group. Moreover the similar (more
arenaceous) physical conditions common to our Devil’s-Bridge bed
and the Gala group may have to do with their having some fossils
im common.
Mr. Lapworth’s researches have established the fact that, in the
Sulurian and Cambrian periods, zones of Graptolites characterize defi-
nite stages, just as do the Ammonites in the Jurassic rocks. But these
latter have their exceptions, and the minor zones are only trust-
worthy within local limits; much more so should we expect this
to be the case with the more lowly organized group of Graptolitide.
The occurrence of Monogr. colonus with Birkhill species in N. Wales
is, indeed, an example of such. On the other hand the stratigra-
phical succession of the Metalliferous slates over the Aberystwyth
nN 2
168 WALTER KEEPING ON THE
erits is clearly marked over a large area, extending from near Borth,
through Aberystwyth, and southwards to Llangrannog*, a gradual
transition between the two groups being everywhereseen. And that
the rocks here occupy their original relative positions is proved by
the position of the raised rock-markings, which are uniformly found
upon the wnder surfaces, as is normal in the lower paleozoic rocks,
whereas when the beds are inverted these structures are found
upon the upper surface.
The only plan of exact harmonization would be, it seems to me,
to suppose that the Aberystwyth grits had died out to the east
before we reach the fossiliferous beds of Morben and Cwm Symlog, —
and older beds had been somehow brought up in the confusion of
folds and synclinals. This may be considered possible; but it
again increases our difficulties in the eastern area (Devil’s Bridge
&c.), where the usual order of the strata persists. I therefore
adhere to my original classification as given in the earlier pages of
this work; for, indeed, the paleontological difficulty is very insig-
nificant.
Comparing the faunas of the Aberystwyth grits and Metalli-
ferous slates, we find that these do not afford any important
data for their separation, but rather demonstrate their intimate
connexion. ‘Twelve of our species of Graptolites are known only
from the Metalliferous slates—namely Rastrites maximus, R. pere-
grinus, Monograptus spinigerus, cyphus, gregarius, intermedius,
runcinatus, and mvolutus, and all the Diplograpt:: but this signi-
fies probably little more than the less favourable conditions for
Graptolitic life in the Aberystwyth grits; for the two rock-groups,
are bound together by the common possession of Monograptus dis-
tans, Clingam, Sedgewickir, crenularis, spiralis, lobiferus, Hisingeri,
and tenuis, and Climacograpsus scalaris. The Orthoceras, Nereites,
Fan-Alge (Buthotrephis), and Nematolites(?) tubularis are also
common to the two groups, and serve further to demonstrate the
paleontological unity of the Aberystwyth and Metalliferous series.
But there is another group (the Plynlimmon group) whose exact
age has not yet been fully considered. ‘These beds contain no fossil
evidence in themselves; but still, from their relations to the under-
lying metalliferous slates and to the more eastern sections, there is
little room for hesitation as to their stratigraphical position.
The underlying rocks are shown to belong to the highest part of the
Lower Llandovery group, or Upper Birkhill series, some of the species
being actually of Gala types. Paralleling, then, our rocks with
those of the south of Scotland, this overlying group of grits must
either be close upon or actually in the Gala and Tarannon group.
We have already seen how the stratigraphical and lithological con-
siderations support the view that they really are an arenaceous
development of the lower part of the Tarannon shale, thus being
the true representatives of the Gala group of Scotland. The asso-
ciated pale slates of Plynlimmon and around Rhyader (Rhyader pale
* There is a difficulty, as before mentioned, at Aberaeron, which I have not
been able thoroughly to investigate. :
GEOLOGY OF CENTRAL WALKS. 169
slates) thus fall into line with the great pale-slate group of Britain
—the Tarannon group.
N.E. Wales.—The Silurian rocks of Corwen, Llangollen, and the
Vale of Clwydd have been described by Prof. T. M‘K. Hughes * ;
and fossils have been collected from the Tarannon shales of the
Conway area by Mr. C. Lapworth, F.G.S. Those species which are
common to our Cardigan rocks are indicated in the Table; but,
besides these, other species, characteristic of newer groups, are
found—namely fetrolites, and Monograptus priodon, colonus, and
galaensis. From these fossils Mr. Lapworth concludes that the
Conway beds “ correspond with the earlier portion of the Gala beds”
of Scotland. Thus the results of paleontology correspond well
with the stratigraphical evidences, which show, in my opinion, that
the great mass of our Cardiganshire series is unrepresented in the
N.E. of Wales (as in the English border counties), or rather that
it is represented by the break which Professor Hughes has worked
out in that district at the base of his Corwen Grit. The black
bands in the Clwydd valley, from which Prof. Hughes obtained
Graptolites, do appear to lie in the parallel of the higher part of
our Metalliferous group.
My friend Mr. J. HK. Marr has just published the details of the
sections at Cerrig y Druidion, N. of Balat. He there finds beneath
the Tarannon shales the equivalent of the Graptolitic mudstones,
containing fossils of the same species as our Cardiganshire series,
but also including Monograptus colonus, which is characteristic
of much higher beds. ‘The section appears to show a greater deve-
lopment of Graptolitic “‘ mudstones ” than in the Clwydd valley, and
so far to represent more fully our Cardiganshire group; but here,
again, as at Corwen, the series appears to be incomplete, because
of the existence of the Silurian unconformity.
General Summary.
Central and West-central Wales is made up almost entirely of a
great series of imperfect slates and Greywackes belonging to our
Cardiganshire group, together with the overlying pale slates and
grits of Rhyader and Plynlimmon. ‘The Cardiganshire group is sub-
divided into the (1) Aberystwyth Grits, and (2) Metalliferous Slates ;
and part of the underlying slates may, perhaps, hereafter be proved
to belong to the same group. Some minor subdivisions are also
distinguishable. The arenaceous rocks are not constant over large
areas, but die out both to north and south.
The rock-beds are astonishingly folded into violent contortions,
with frequent inversions, especially in the Metalliferous series, so
as often to produce the misleading appearance of a regular and
continuous ascending series exceeding five miles in thickness, All
the important axes of elevation in the country havea common N. and
S. direction, two of the main folds being the Aberystwyth anticlinal
* Quart. Journ. Geol. Soc. vol. xxxiii. p. 207, vol. xxxv. p. 694.
t Ann. Nat. Hist. 1880, vol. ix. p. 49.
$ Quart. Journ. Geol. Soe. vol. xxxvi. p. 277.
170 ON THE GEOLOGY OF CENTRAL WALES.
and the Plynlimmon synclinal. Secondary axes of upheaval bring
up the lower beds of the series at the Devil’s Bridge and near Cwm
Symlog. Innumerable minor foldings preserve the same north-and-
south strike.
The included fossil remains, especially the Graptolites, prove the —
Aberystwyth Grits and Metalliferous Slates to belong to the same
general geological horizon—namely, on the parallel of the upper
Birkhill series of 8. Scotland and the Coniston “‘ Mudstones” of the
English Lake district. The Plynlimmon Grits are probably an
arenaceous development of the Tarannon Shales; and the Cwm-Hlan
conglomerates and Rhyader Pale Slates belong to the same series.
Following up our Cardiganshire series to the lines of junction
with older and newer groups in parts of Montgomeryshire, South
Cardiganshire, Caermarthenshire, and Merioneth, we find no evidence
of a break in any part of the rock-groups; but there 1s concordant
evidence of lithological passage from the Bala to the Llandovery
groups, and from these upwards into the Tarannon Shales and the
Denbighshire Grit series. On the contrary, in Denbighshire and
N.E. Merioneth, Professor Hughes has shown that, just as in the
English-Welsh border districts, there is an important stratigraphical
break at about this Llandovery period. Now the beds below that
break in N. Wales are the Bala group, i. e. inferior to our Cardigan-
shire series; those above it are basement-grits and conglomerates
(the Corwen Grit), covered by the pale slates, with some black
Graptolitic bands. These latter contain some species In common
with the Cardiganshire group, but also others characteristic of a
higher horizon than our fossiliferous beds.
Thus all the facts are harmonious in pointing to a continuity of
the Silurian and Cambrian deposits in West and Central Wales,
while an important break exists in the east and north-east. Our
Cardiganshire group is only partially developed (its upper part) in
the latter district, being, in fact, there represented by a great strati-
graphical break—Sedgwick’s original May-Hill unconformity.
I conclude that, while in the latest Cambrian times(Sedgw.) and the
dawn of the Silurian era the elevatory forces, acting in a north-and-
south direction, lifted up the sea-bed to form a land-surface over the
west of England and the Welsh borders, these forces influenced the
greater part of Wales only in a less degree—producing, it may be,
the shallower water in which the Aberystwyth grits were laid down,
but not interfering with the continuous deposition of sediment and
the unbroken sequence of the geological record from the Cambrian
to the Silurian eras.
te ceee
.
:
N
Lance showing Distribution of Fossils in Central Wales. [fo fitce page 170.
Specimens marked thus (+) have been identified by Mr. O. Lapworth, F.G.S,
ee
: Scotland. Goniel
| 4 $ 7 E 3 5 : o a 2 ack , es = = loniston
a =) =) . = BS |e sc bb gb gE 2 = F Mudstones. | =
SS SE eS Me Sle | ES d S/ = |da/ 2/3 |ae| 2 | 2 ae
= (=) y s = i el =| BD 5 iS) is} & Er Gi |f dg a ] fs
= = f is} e |Ce § 5 a: S 2 [2] A 5 3 6
Sst | el is] Se ee ep eta 2 Bs SRS elle eee a a. WE Ale
SS eee ee hee 2 (ee |e ca |e E/E) e] 2 lee} | & [te] 6 | 2] es | Bele
3 o S$ = 5 2A gy]
SSPE ES ads (Euston ae | ae (ee 8 |e ee ee ee se ie
=
we eres pi saesee: [eeeeee fiimesene [i CHES {| SE eeseee [ii seuwen || cuncne | cvauen f susece | savese | (senses | srene * * *
mf | feces iceewee | Pf YP ceecce | ceceee | | wevene | ceeeee fi ceeeee | ccceee | ceceen | ceesee | teneee | cesses *
S| eee | aaa | A eseeadl|eseeeod lessees
Sef I cee leanne |i eecea eeeno lll Seeeee [ic osewn) || wecurn | vecees ||| eeene= | uunmac'G ccvses | eevee | secone | cevene *
1} Be *
; J rere)
* MH cecece
Ho] wacees *
MO oceeece *
*
* 2
= * .
* |
« |
* | HO osneene
* .
en l(encceceul| Gastipe
Hf ewaee | cervee
* *
*
el
| ee ee eee
. an eter Ts *
2 * *
* * *
* * .
— << i *
ee ‘ conece: | herrecoe |) ceooce | acetce: |) atacos 1} cocece ?
Nemeriies Obvantii, Murch,
> *
Tertoerrs.
Calymene. sp.
coerey ¥
| |
Bs ass |. serene Wiesarecd|it-cssmillsrenee | teraction | [tensor || tsaseas oh lWhecerxo *
oP ecco *
esacee toe A peek | recap Woseree 2 WN eeeceadd| nccee \Weeeepe | ecacce || cone |) Goch *
| Gala Group.
Z
* Confined to the highest 1 nari
Pageant Dae pata qu she Br Birkhill of South Scotland eae ° A few fraginents only in the highest seams of U, per Birkhill (Lapw.),
2 Known only in ee Birkhill bed Shale and its equivalents (Lapw,), ° M, runcinatus is peculiar to Upper Birkhill Shales Lapw,).
* Restricted to a single zone in the Te Moffat and Girvan (Lapw.), 7 Makes its first appearance in middle of U: per Birkhill (Lapw.)
oper Birkhill Shales (Lapu.). * Diployrapsus Hughesié is confined to the Upper Birkhill Shales (Lapw.).
Quart. Jour. Geol. aha Volo ea ae
Mintern Bros. imp.
INES Hoomdeliti
WELSH CLADOPHORA.
ON SOME NEW SPECIES OF CLADOPHORA. 171
APPENDIX.
On the Cravopnora (Hopk.) or Drenproip GRaprorirss collected by
Professor Kuxpine in the Llandovery Rocks of Mid Wales. By
Cuas. Lapwortu, Esq., F.G.8. &e.
[Puate VII.|
Tse forms of Cladophora collected by Professor Keeping from
the Llandovery rocks of Cardiganshire are, regarded collectively, of
a type almost new to British paleontology. “Although intimately
allied to the well-known dendroid species of the Quebec and Arenig
formation, they are very distinct in their minor features. They are
essentially of a Silurian (Upper) facies, and they remind us strongly
of a group recently made known to us through the researches of Mr.
Spencer, of Toronto, which characterizes the Clinton and Niagara
Groups of New York and Upper Canada *.
None of our examples shows the complete polypary, or affords dis-
tinct proof of the presence of all the more minute classificatory
features ; but there is satisfactory evidence of the presence of at
least four distinct genera and seven species. The genera repre-
sented are Dictyonema, Hall, Calyptograptus, Spencer, -Acantho-
graptus, Spencer, and Odontocaulis, Lapw. Dictyonema is a well-
known British genus; the remainder are new to British paleon-
tology. Calyptograptus and <Acanthograptus have been already
briefly noticed from American strata by Mr. Spencer, but have not
hitherto been figured. Odontocaulis is a new genus, of a peculiar
type.
: Of the seven distinct species recognizable, four (viz. Dictyonema
corrugatellum, Calyptograptus plumosus, C’. digttatus, and Odontocarulis
‘Keepingw) are as yet peculiar to the Mid-Wales area. The remaining
three have already been recognized by myself in the Silurian rocks
of the south of Scotland. Dictyonema venustum certainly occurs in
the Upper Gala group of Selkirkshire (Llandovery-Tarannon), and
doubtfully in strata of a little older date in the Girvan area.
Dictyonema delicatulum has been met with in the Llandovery (Lower)
of Shalloch Forge, near Girvan. Acanthograptus ramosus occurs
also im the Girvan area, at the base of the representative of the
Tarannon Shales.
We do not yet know enough of the Cladophora of North America
to enable us to identify any of these Mid-Wales forms with corre-
sponding species already described or figured from the Silurian strata
of that continent.
Genus DictyoNnEMA.
Dictyonema, Hall, Paleontology, New York, vol. ii.
1. DicryoNEMA VENUsIUM, sp. nov. Plate VII. figs. la—le.
Polypary cyathiform in the growing state, at least 10 inches in
- transverse diameter. Branches uniform, about one eightieth of an
* “Graptolites of the Niagara Formation,” by J. W. Specs, F.G.S8., Canadian
Naturalist, 1878-9, pp. 457-463.
172 C. LAPWORTH ON SOME NEW
inch in transverse diameter, radiating from the centre with few and
remote bifurcations; approximately parallel distally; having 25
branches to the inch, connected by frequent capillary dissepi-
ments 12 or 13 to the inch. Calycles biserial, closely adpressed to
the polypary, 50 to the inch; apertural margin acute, rarely spinose.
The largest specimens obtained are distal fragments of the
polypary, about two inches in length ; and from the characteristics
presented by these fragments the foregoing diagnosis has been
drawn up.
This form is undoubtedly new to British paleontology. It may,
however, be proved in the future to be identical with some of the
imperfectly known American forms from the Clinton and Niagara
eroups.
~ Locality, Llandovery of Devil’s Bridge, Aberystwyth. Dictyonema
venustum is a rare fossil in the Llandovery rocks, of the south of
Scotland, at Abbotsford, Winterhope, and Penwhapple Glen.
2, DicrYoNEMA DELICATULUM, sp. nov. Plate VII. figs. 2a, 26.
Polypary cyathiform ? probably three or four inches in transverse
diameter. Branches 40 to the inch, about 54, of an inch in
width, distally parallel, connected by indistinct capillary dissepi-
ments 16 or 17 to the inch; bifurcations? Calycles biserial, 80 to
the inch ; aperture horizontal, devoid of ornament.
The best example of this species collected is shown in the figure,
Plate VII. fig. 2a. . The characters it presents show that it
belonged to a distinct species from that already described, from
which it differs mainly in the narrower and more closely-set
branches, and in the more numerous calycles and dissepiments.
Horizon and Locality. Llandovery of Bryn y Carnau, Aberyst-
wyth.
a single specimen has also been collected from the Pentamerus-
beds of Shalloch Forge, Girvan, South Scotland.
3. DicTYoNEMA CORRUGATELLUM, sp. nov. Plate VII. figs. 3a, 36.
Polypary cyathiform, about one aud a half inch in height. The
branches are nearly parallel, about ;}5 of an inch in diameter, and
zis of an inch apart, connected by fine transverse dissepiments at
regular distances of about =, of an “inch, undulating in direction, the
edees being thrown alternately from side to side by the projection
of the outer margin of the calycles. Calycles 120 to the inch,
alternate, with gibbous outer margin, and deep rounded aperture
lying interior to the edge of the branch.
The most striking feature of this elegant little species is formed
by the wrinkled or undulating outer edges of the branches, which
wave from side to side owing to the projection of the ventral
margin of the calycles. The slender branches divide more
frequently than is the case with the generality of species of
Dictyonema ; and the transverse dissepiments are stouter and appa-
rently polypiferous.
The calycles have their apertural margin strongly introverted,
SPECIES OF CLADOPHORA. LS
in the manner of those of Dicellograptus, Hopk.; and the line
of the aperture lies wholly within the ventral margin of the
branch.
Horizon and Locality. Llandovery of Devil’s Bridge, Aberyst-
wyth, Cardiganshire. Collection of Dr. Humpidge, Aberystwyth.
Genus CALYPTOGRAPTUS.
Calyptograptus, Spencer, Canadian Naturalist; 1878-79, p. 459.
“Gen. char. Polypary cyathiform, with numerous bifurcating
branches, which are dichotomous at the termination, but are not
connected by lateral processes. The branches are marked with
strie resembling rhomboidal pits; the axis has a black corneous
exterior; and the radicle is composed of a thickened mass of the
same texture as the branches. In appearance and texture this genus
resembles Dictyonema; but the branches are all independent, not
being connected by transverse dissepiments as in that genus, and are
only united in one mass at the root” (Spencer, loc. cit.).
One of the Cladophora collected by Professor Keeping appears to
possess many of the foregoing characters, which are given by Mr.
Spencer as the peculiarities of his genus Calyptograptus. ‘There are,
however, some marked distinctions between our species and his
typical examples; nevertheless it is most undoubtedly a closely
allied form, and may therefore most conveniently be provisionally
placed in this genus until we know more of the proper generic
distinctions of these obscure fossils.
4, CaLYPTOGRAPTUS? PLUMOSUS, sp.nov. Plate VII. fig. 4.
Polypary cyathiform?, in the growing state, about one inch and
a half in height, composed of numerous bifurcating polypiferous
branches united into a short stem, longitudinally striated, not
connected by transverse dissepiments. Calycles closely arranged,
biserial. Basal disk elliptical in form, about one fourth of an inch
in diameter.
The stem, which is very short and stout, rises from the centre of
the basal disk, and divides for the first time within about one eighth
of an inch of its origin; the second, third, and fourth subdivisions
are about one tenth of an inch apart; the later bifurcations are a
little more remote. The primal branches are about one thirtieth
of an inch in diameter ; the final branchlets are almost capillary.
The substance of the polypary appears to have been somewhat
membranous in character, and is wrinkled or striated longitudinally
in the fossil. Two series of calycles are just discernible in the
proximal portions of some of the branches, their apertural margins
being éxhibited as short slits crossing the branches transversely,
almost at right angles to their general direction.
This form agrees with Dictyonema and Callograptus in the regular
dichotomous nature of the method of subdivision of its principal
branches. It differs, however, most markedly from both these
genera in the apparent absence of the transverse dissepiments
174 Cc. LAPWORTH ON SOME NEW
uniting the branches. In the mode of branching and in the form of
the calycles it approaches the genus Odontocaulis, to be presently
described, from which, however, it is easily separated by its short
non-polypiferous stem.
Horizon and Locality. Llandovery of Devil’s Bridge, Aberyst-
wyth.
5, CALYPTOGRAPTUS? DieiTaTUS, sp. nov. Plate VII. figs. 6a—6b.
Polypary short, composed of numerous compound branches about
roy of an inch in width, dividing irregularly, and terminated distally
by a group of palmatifid branchlets about one tenth of an inch in
length. Calycles of the type of those of Callograptus, about 50 to
the inch.
The magnified drawing gives a fair idea of the external features
of the only specimens seen, which are mere fragments. The
proximal extremity of the stem is unknown; but the irregular mode
of subdivision of the branches is different from what generally
occurs in Dictyonema and its allies. There is a doubtful appearance
of reticulation among the secondary branches.
The most remarkable feature of this form is the strange digitate
character of the final spine-like branchlets. Mr. Spencer has noticed
the same feature in the genus Rhizograptus (op. cit. supra, p. 461),
to which itis possible the present species properly belongs.
Horizon and Loculity. Llandovery of Devil’s Bridge, Aberyst-
wyth.
Genus ACANTHOGRAPTUS, Spencer.
Gen. char. “ Polypary shrublike, consisting of thick branches,
principally rising from near the base, with little divergence and
some bifurcations. One side of the branches is furnished with
prominent spines or denticles, which appear to mark the cell-
apertures. Test corneous and indistinctly striated.”
‘«« This generic form resembles Dendrograptus, but is stronger and
more bushy than species of that genus, and has conspicuous spines
indicating a different cell-structure ” (Spencer, op. cat. p. 463).
The foregoing is Spencer’s diagnosis of his new genus Acantho-
graptus. I have provisionally assigned to it one of Professor
Keeping’s species, which answers fairly enough to Spencer’s defini-
tion. It is impossible to ascertain from Spencer’s diagnosis whether
the denticles that ornament the calycles are horizontal or inclined.
if the former be the case, I suspect that Acanthograptus will be found
to lie somewhere near Thamnograptus of Hall, in which the calycles
are provided with long projecting spines, and that the present form
must be regarded as the type of a new genus.
Acanthograptus occurs both in the Bala and Llandovery strata
of Girvan, South Ayrshire, where, however, it is an uneommon
fossil. None of the species collected by myself from the Scottish
locality appears to be precisely identical with the Mid- Wales form.
6, ACANTHOGRAPTUS RAMOsUS, sp. nov. Plate VII. fig. 5.
Polypary short, shrublike, with thick rigid branches, repeatedly
SPECIES OF CLADOPHORA. WG
and irregularly branching and rebranching. Base unknown. Calycles
monoprionidian ?, often with long acute denticles, which have an
ascending direction.
We have only one fair example of this genus from the Mid-Wales
beds; and the foregoing characters are all that can be made out.
The height of the visible portion of the polypary is less than half an
inch. The main branches are apparently about one fortieth of an inch
in diameter below, and are strongly striated throughout the whole of
their extent. The right-hand branch, which is the better preserved,
throws off three secondary branches in the upper half of its length.
These secondary branches are of various lengths, being so extended
that their outer terminations are on, or about, the same level. Each
secondary branch splits at its summit into two secondary branchlets
or polypiferous spines, about one twentieth of an inch in length,
and terminating outwards in a short, stiff, mucronate point. The
remaining primary branches present essentially the same general
features.
One margin of the branches exhibits small denticulations at short
and regular intervals (about 50 to the inch), marking the mouths
of the calycles, the margins of which are usually concave. The
outer angle of the aperture is sometimes very slightly projecting and
more or less rounded off, as in the genus Dictyonema. Generally,
however, the outer margin of the aperture is prolonged into a stout
denticle, which stretches outward and upward at an angle of about
45 degrees to the main axis of the branch, and is terminated in
a blunt point; the inner margin of the calycle, shown by a little
groove upon the surface of the branch, running for some distance
almost parallel with the outer margin.
The colour of the test is black, and the texture corneous.
Horizon and Locality. Llandovery of the Devil’s Bridge, Aberyst-
wyth.
ODONTOCAULIS, gen. Nov.
Gen. char. Polypary cyathiform, composed of numerous indepen-
dent and frequently bifurcating polypiferous branches, originating
from the distal extremity of a short stem, which is likewise poly-
piferous, and is terminated proximally in an irregular corneous
expansion. Hydrothece of the type of those of Dictyonema,
biserial, subalternate.
The chief peculiarity of this genus is afforded by the character of
the stem, which is identical in every respect with the main branches,
and, like them, is denticulate or polypiferous throughout the whole of
its extent. It commences proximally in a flattened expansion, with
irregular or frayed-out edges, possibly the remains of a disk or bulb
of attachment.
The mode of branching is rigidly dichotomous, the first two
branches being formed by the subdivision of the main stem itself.
Each arm branches and rebranches again and again in the same
manner, at irequent and close intervals,-composing an elegant cyathi-
form or fanlike polypary, very symmetrical in form. The branches
retain their original width to their final division, which gives rise to
two minute branches less than one tenth of an inch in length.
176 C. LAPWORTH ON SOME NEW
The hydrothece are more prominent than those upon Dictyonema.
The distal extremity of each appears to have been free and slightly
introverted, as in the majority of the bilateral family of the
Dicranograptide.
Odontocaulis is separated from Dictyonema by the absence of the
transverse dissepiments, and by the polypiferous character of the
stem. From Callograptus, which it much resembles, the same
features effectually distinguish it. In Dendrograptus the stem is
stout and devoid of polypes, while the branches are irregularly
disposed ; in the present genus the stem is no thicker than the
branches, is polypiferous, and the branches are regularly and
symmetrically subdivided. It has probably its nearest ally in
Rhizograptus (Spencer, ‘ Canadian Naturalist,’ 1879, p. 460); but in
that genus the stem appears to be barren, and the branches are
possibly united at intervals.
7. OpontocavLis KEEPINGII, sp. nov. Plate VII. figs. 7a, 70.
Polypary composed of numerous elegant flexuous branches,
frequently divided and subdivided in a regularly dichotomous
manner, originating from the distal extremity of a polypiferous
stem about one fourth of an inch in length, and forming a
cyathiform frond one inch and a half in height. Hydrothece 50
to the inch, free, distally patulous ; aperture prolonged, introverted ;
denticle obtuse, rarely spinose.
In the only specimen coliected the polypary commences proximally
with a flattened expansion or disk with irregular or frayed-out
edges. The stem is curved ventrally, and bears a single series of
hydrothecze, which are most distinctly shown. There are also indi-
cations of a second series. These hydrothece are a little more widely
separated than those upon the branches, and appear to have been
stronger and more projecting. At its summit the stem divides into .
two, originating the primary branches. Within one twentieth of
an inch of their origin each of these again divides in a correspond-
ing manner. Within the next tenth of an inch the branchlets
are again subdivided, and so on till as many as six of these
dichotomous divisions have been made. The terminal branchlets
are very short, less than one tenth of an inch in length; but they
are polypiferous to their visible extremities.
The hydrothecz upon the branches average about 55 or 60 to the
inch. The majority are seen as scaliform impressions; those
visible in profile are not unlike those in Dicellograptus, Hopkinson.
The branches are of subequal diameter throughout, about one
fortieth of an inch. They are quite free and independent, neither
inosculating, asin some forms of Dictyonema, nor being connected
by transverse dissepiments, as in that genus and its ally Callo-
graptus.
This beautiful little species is dedicated to its discoverer, Professor
Walter Keeping.
Horizon and Locality. Llandovery of Devil’s Bridge, Aberyst-
wyth, Cardiganshire.
SPECIES OF CLADOPHORA. 177
- EXPLANATION OF PLATE VII.
Fig. 1. Dictyonema venustum, sp.nov.: 1 a, natural size; 10, magnified 10 dia-
meters. Locality: Devil’s Bridge, Aberystwyth (coll. W. Keeping).
1 ¢, nat. size. - Loc.: Williamshope, Gala group (coll. C. Lapworth).
2. Dictyonema delicatulum, sp. nov.: 2a, nat. size; 26, magnified 10 dia-
meters. lLoc.: Bryn y Carnau (coll. W. Keeping).
3. Dictyonema corrugatellum, sp.nov.: 3a, nat. size; 3b, magnified 10 dia-
meters. lLoc.: Devil’s Bridge (coll. Dr. Humpidge, Aberystwyth).
4. Calyptograptus plumosus, sp. noy.: nat.size. Loc.: Devil’s Bridge
(coll. W. Keeping).
5. Acanthograptus ramosus, sp. nov.: magnified 3 diameters. Loc.: Devil’s
Bridge (coll. W. Keeping).
6. Calyptograptus digitatus, sp.noy.: 6 a, nat. size; 66, magnified 5 dia-
meters. Loc.: Devil’s Bridge (coll. W. Keeping).
7. Odontocaulis Keepingit, gen. et sp. nov.: 7 a, nat. size; 7 4, basal por-
tion magnified 5 diameters. Loc.: Devil’s Bridge (coll. W. Keeping).
Discussion.
The Presipenr said that the paper was an important contribution
to the geology of Mid Wales. The fossils were interesting and
remarkable, especially the Graptolites.
Prof. HueHEs pointed out that the North-Wales Silurian was
quite different from that of South Wales, and that the area described
by the author was far from the typical sections of either north or
south and differed from both. He considered the paper a valuable
contribution to our knowledge.
Dr. Hicks was glad to hear that in this area also, as in Pembroke-
shire, there was no break between the Upper and Lower Silurians.
It was also satisfactory to see that fossils had turned up on
examination in these rocks, formerly reported to be barren or
nearly so.
178 G. W. SHRUBSOLE—-FURTHER NOTES ON
13. Further Notes on the CARBONIFEROUS IENESTELLIDE. By GuORGE
Wau. Surussore, Hsq. F.G.S. (Read January 19, 1881.)
In a former communication to the Society L endeavoured to show
that, as the result of a careful comparison of the existing individual
forms, as figured by previous describers, with some tolerably
perfect specimens in my own possession, it would be necessary to
redescribe the species of Wenestella and considerably reduce their
number. I accordingly append a redescription of the more promi-
nent species ; but before introducing that, it will be necessary to say
something about the foundation of the genus Menestella, since it can
readily be imagined that the same causes which have thrown con-
fusion into the species, have tended also to obscure the genus—
namely the fragmentary and imperfect state of the specimens ex-
amined, and the want of attention to the stages of individual growth
and other details. Accordingly I find the existing descriptions of the
genus Menestella inaccurate in many essential details. The genus
has been defined by several paleontologists, but each time with
reference to the fossils of a particular period; and no one description is
sufficiently comprehensive to embrace all the members of the family
Fenestellidee as they occur in the various Palseozoic formations. A
fresh description of the genus therefore appears to be desirable.
Without entering upon a full history of the genus Fenestella, I
may mention that the first to describe it as such was Lonsdale, in
1839*, who adopted the name from the MS. of Miller of Bristol,
who had been engaged on a work on the Corals of the Mountain
Limestone, which he did not live to complete. He gave the name
Fenestella to the lace corals. enestella Millert of the Silurian is
so named after him. Lonsdale twice defined the genus—first in the
‘Silurian System,’ and again in the ‘ Geology of Russia’r. In the
former he restricted the cells to one row on each side of the keel :
and in the latter he placed no such limit to the order or arrangement
of the cells ; hence it included Polypora, Retepora &c., in fact all the
fenestrate species. His otherwise elaborate definition was also
faulty to the serious extent that he described the appearance of a
common incrusting coral as the mature growth of the Menestella.
This [ explained in a recent communication to the Society.
Phillips next in order of time (1841) gave a very good description
of the genus, so far as relates to the Devonian groupt; but much vf
its details are not applicable to the Silurian group.
Prof. M‘Coy, in 18448, restricted the genus to forms with two rows
of pores on the branches, so as to include only the true Lenestelle.
The pore-cells he limits to the external face, whereas in the majority
of the species they are on the inside of the polyzoary. He further
x Murchison’s ‘Silurian System,’ p. 677.
t Geology of Russia, vol. i. Appendix A, p. 629.
t Paleeozoic Fossils, pp. 22, 25.
§ M‘Coy’s Syn. Carb. Foss. Treland, p. 290.
THE CARBONIFEROUS FENESTELLIDZ. 179
states that the perfect condition of Fenestelia will be found in his
genus Henutrypa. ‘This latter I have shown* to be a mistake due
to an incrusting organism on Jenestella membranacea, Phil.
In his second definition, in 1854 ++, which was intended to include
both Carboniferous and Silurian species, M‘Coy is more successful ;
no mention is made of the particular face on which the cells are
placed. He does not adequately describe the shape of the polyzoary,
and adopts one of Lonsdale’s errors respecting a layer of vertical
capillary tubes on the reverse face.
The last definition we have was by Prof. King t in 1848, after
arranging the Permian Polyzoa. He ignores M‘Coy’s work in
1844, and says that the genus, as constructed by Lonsdale in 1845,
requires subdividing. As no trace of the incrusting coral was found
in the Permian species, all reference to Lonsdale’s supposed mature
condition of the Fenestella is omitted. Prof. King’s short and other-
wise exact account is inexact in stating that the cells are distributed
in two or more linear series.. The true Fenestclle have never
more than two rows of cells on the interstice ; the supposed row on
the keel does not really consist of cell-pores, but of the bases of hollow
Spiny processes, which oftentimes, in the case of the Permian /ene-
stelle, have been unduly distorted by a subsequent deposition of
carbonate of lime.
From the foregoing it is evident that none of the origina] deseri-
bers of the genus Fenestella has grasped the main features of it as
a whole. What is wanted is a definition which shall embrace the
whole of the Paleozoic Menestelle.
The following definition is therefore proposed, after a careful study
of the several species ranging from Silurian to Carboniferous times.
Genus FrnEsTELLA, Lonsdale.
Polyzoary a calcareous reticulate expansion, either flat, conical,
or cup-shaped, formed of slender bifurcating branches (interstices),
poriferous on one face, connected by non-poriferous bars (dissepi-
ments) forming an open network. Ced/s immersed in the interstices,
and arranged in two longitudinal rows divided by a central keel, on
which are often prominences. Cell-mouth small, circular, and
prominent when preserved.
FENESTELLA PLEBEIA, M‘Coy, Syn. Carb. Foss. Ireland, p. 29,
fig. 3.
Fenestella antiqua, Lonsd., M‘Coy, Syn. Carb. Foss. Ireland,
p. 200. |
carinata, M‘Coy, Syn. Carb. Foss. Ireland, pl. 28. fig. 12.
devonica, Semenow et v. Moller, Bull. de l’Acad. de St.
Pétersbourg, t. vii. p. 233, pl. 3. fig. 16.
formosa, M‘Coy, Syn. Carb. Foss. Ireland, pl. 29. fig. 2.
flustriformis, Phill. Geol. Yorkshire, pl. i. figs. 11, 12.
fossula, Lonsd., Darwin’s Obs. on Volcan. Isl. p. 166.
* Quart. Journ. Geol. Soe. vol. xxxv. p. 282.
t Brit. Pal. Foss. p. 49. ¢ Permian Fossils. p. 34.
180 G. W. SHRUBSOLE—-FURTHER NOTES ON
Fenestella fossula, Dana, Geol. U.S. Explor. Uxped. p. 710, pl. 1.
fig. 3.
**___ nlebeia, POrbieny, Prod. de Paléont. strat, t. i. p. 152.
—— irregularis, Phill. Geol. Yorkshire, pl. 1. figs. 21, 22.
—— retiformis, Schloth., King’s Perm. Foss. pl. 2. figs. 8-19.
—— trituberculata, Prout, Trans. Acad. St. Louis, vol. 1. p. 228.
— undulata, Phill. Geol. Yorkshire, pl. 1. figs. 16-18.
—— virgosa, Kichwald, Lethea Rossica, tom. 1. p. 358, pl. 23.
9
Sp. char.—Polyzoary a flat expansion, slightly convoluted, circular
or oval in outline, depressed in the centre, by which it is attached.
Interstices regular on the obverse face when well preserved, somewhat
rounded otherwise, sides angular, keeled. Drsseprments thin, expand-
ing at junction with interstice, more markedly on obverse than re-
verse face. enestrules regular, oblong, equal to width of interstice
on obverse face, twice the width on reverse face ; four in the space of
two lines longitudinally, and six fenestrules in the space of two lines
transversely. Acel rounded and strong, with two or three nodes in
the length of a fenestrule. Pores round, prominent, their diameter
apart, two or three in the length of a fenestrule, and often one more
prominent than the rest in the angle formed by the junction of the
dissepiment with the interstice.
Obs. This species, whether from Scotch, Irish, or English localities,
is everywhere the predominant form of Menestella. It attained to
the largest expansion of polyzoary of any of the species. It de-
serves in every way to be regarded as the typical species of the
Carboniferous varieties. I have traced its growth through all its
stages, from a speck with two interstices on a stalk which clasped, it
might be, the spine of a Productus or a fragment of Serpula, to the
adult form with its strong and numerous rootlets. The early leaf-
like growth on a footstalk soon underwent a change; the footstalk
became one of many rootlets, and the polyzoary coralliform at the
base, and ultimately a more or less circular expansion, the edges of
which terminated in slightly convoluted lobes. Its attachment to
the rock was secured by a cluster of rootlets from about the base,
and, indeed, from any part of the polyzoary which offered convenience
of attachment.
The actual size to which this species attains it is difficult to
estimate, owing to the cleavage of the shale in which it occurs. I
have seen indications which lead me to believe that an adult poly-
zoon might attain a diameter of nearly two feet. Specimens of
this species will be found to differ from each other somewhat in
appearance. ‘This I have found is more owing to the nature of the
matrix in which it has been imbedded than to any other cause.
The more calcium carbonate present in it, the fuller and more life-like
the organism appears, while it is flat and shrunken in the ordinary
black aluminous shale of the Carboniferous beds.
In diagnosing the species the first thing to be noted is the size of its
interstice, in which it is intermediate between Fenestella nodulosa,
THE CARBONIFEROUS FENESTELLID&. 181
Phill, and Lmestella polyporata, Phill. There is also a peculiar
smoothness and regularity, in the growth alike of interstice and
dissepiment, which is attained by none of the other species and is
a distinguishing mark. The presence of three or four pore-cells in
a given space, the dissepiments, and the oblong fenestrules complete
the identity. Prot. M‘Coy’s fine drawing of this species: is taken from
a partly worn-down specimen in which the sides of the interstice have
become sharp and angular, and the keel scarcely visible; whereas the
interstice should have been full and rounded, and capped with a ridge
or keel, bearing the remains of spiny projections, while on either side
the cells stood out prominent and free. ,
There is no doubt about the identity of this species with Gorgoma
antigua, Goldt., although his figure is drawn from a much weathered
and mutilated fragment. Tt also agrees with Fenestella retiforinis,
Schloth., the leading Permian species. Jam aware that a contrary
opinion has been expressed. Virtually the species are the same.
Phillips was, in this country, the first to give a descriptive account
of it. His Menestella wreqularis, F. undulata, and F. flustriforimis
are all different portions of the polyzoary, under somewhat varying
conditions of growth and preservation. I cannot agree with Prof.
M‘Coy in assigning Fenestella flustriformis to Ptylopora» flustri-
jormis. As figured by Phillips, it is only the cast in limestone
of the reverse face; and, as such, its relationship to Ptylopora
is purely conjectural. Prof. M‘Coy was the first to recognize the
importance of this species, and to do justice to it in ‘the way
of description; and hence, although not its author, that it should
retain the name which he gave to it is eencrally conceded. In
this view I am borne out by Prof. de Koninck, who states ‘+ that
Lonsdale was the first to describe this species as Fenestella fossula,
but that his description was incomplete, and insufficient to recognize
it with certainty, whilst M‘Coy’s description was full and accurate’ oe
Phillips’s notice of it some years prior to that of Lonsdale was even
more incomplete. For the foreign synonyms of Menestella plebeia
I am also indebted to Prof. de Koninck’s work on the Carboniferous
Fossils of New South Wales.
FENESTELLA MEMBRANACEA, Phil. Geol. Yorks. pl. i. figs. 1-6.
Fenestella flabellata, Phill. Geol. Yorks. pl. i. figs. 7-10.
henuspherica, M‘Coy, Syn. Carb. Foss. Irel. pl. xxix. fig. 4.
—— Shumardiu, Prout, Trans. Acad. St. Louis, p. 232.
tenurfila, Phill. Geol. Yorks. pl. 1. figs. 93, 24, 25.
Sp. char.—Base cylindrical, tapering to a “fine point, vw with strong
non-poriferous rootlets attached. Upper part widely expanded.
From nine to twelve inches in length, and five to eight ches in
width. Jnéerstices rounded, straight, in parallel lines, keeled. Dis-
sepiments fine, shghtly expanded at junction with interstice. Henes-
trules oblong, slightly wider than insterstice, from two to three times
as long as wide. At one inch from base, five dissepiments in the
space of two lines measured vertically, and eight dissepiments in.
* Hoss. Pal. Nouy. Galles du Sud, 1877.
Q.J.G.8. No. 146. 0
182 G. W. SHRUBSOLE—-FURTHER NOTES ON
two lines transversely. Fenestrules gradually increasing in size
with the growth. Pores small, round, more than their own diameter
apart, placed on the outer face of the polyzoarium. At the base
three pores within the length of a fenestrule ; in the upper portion
four in the same space.
Obs. There are many points of considerable interest attaching to
this species. In shape and appearance it is an enlarged type of
the Silurian species generally, and particularly of my Fenestella
lineata. It is the only representative of the old type which has
survived to Carboniferous times. In addition to its shape, it has
most of the features of its prototype, viz. interstices seldom bifurca-
ting, proceeding in parallel lines, and pores on outer face of polyzoary.
Its early growth, from a minute point, was a tapering, often curved
root-base, from which grew a hollow and gradually widening cone,
which ultimately expanded in slightly folded and lobed outlines
around the aperture. ‘To secure in position so fragile a structure,
numerous solid rootlets grew from various points of the base, and
attached themselves to surrounding objects. Being somewhat cylin-
drical, 1t did not need to make the usual amount of lateral growth
by bifurcation, as in the ordinary open type of Carboniferous
enestelle. Owing to this comparative absence of bifurcation in
the insterstice, its lines are singularly regular, forming a series of
parallel rows. Further, its lateral growth was obtained by a gradual
enlargement of all parts of the structure, proceeding from the base
upwards—so much so that while at the base four fenestrules may be
counted in one line, at the distance of two inches there are only two
in the same space, thus doubling the circumference of the polyzoary
without the aid of division of the interstice. This enlargement in
the growth is more or less persistent throughout the polyzoarium,
but not to the same extent, and furnishes at once a key to the
synonyms. Accompanying the increased growth, an additional
pore-cell may be noticed between the dessepiments. ‘Thus the
difference between the base and the upper portion, both as to size
and shape, is of a very marked character, and quite accounts for the
several species into which this one has been divided. Phillips was
the earliest worker at it; he named the extreme base VFenestella
membranacea, the upper and enlarged growth Fenesiella flabellata,
and the more delicately formed and intermediate portion Menesiella
tenurfila. 3 :
I have alluded to the fact that in the more cylindrical portion of
FF’, membranacea bifurcation of the insterstice was arrested in part.
At times a variety of circumstances may have hindered the longi-
tudinal extension of the polyzoary ; then we find a rapid bifurcation
which gives a globose outline to the expansion, and the form is then
the Ff. hemispheriea of M‘Coy, while all its other details as to the
pores, interstices, &c. clearly point to its identity with /. membra-
nacea, Phill.
The only species likely to be confounded with the foregoing is the
F, nodulosa of Phillips. The square form of the fenestrule in the
latter will at once indicate its character.
THE CARBONIFEROUS FENESTELLID2:. 183
Locality. This species is comparatively rare in the Mountain-
Limestone beds of England and Scotland, and very abundant in
certain localities in Ireland.
FENESTELLA NopuLosA, Phill. Geol. Yorks. pl. i. figs. 31, 32, 33.
Fenestella bicellulata, R. Kth., Jun., Mem. Geol. Surv. Scotl. Sheet
Bo, p. 101. :
—— fruiex, M‘Coy, Syn. Carb. Foss. Ireland, pl. xviii. fig. 10.
— Popeana, Prout, Trans. Acad. St. Louis, p. 229.
subretiformis, Prout, Trans. Acad. St. Louis, p. 233.
Sp. char.—Polyzoarium, early growth foliaceous, having a distinct
stem or footstalk, becoming an oval or circular expansion. Jnter-
stices regular, rounded, carinated and bifurcating ; remains of spiny
processes along the keel. Dussepiments thin, rounded, regular, a
little arched in the early stage, not so thick as interstices. enes-
trules square, regular in the early growth, four fenestrules in the
space of one line measured longitudinally, and four fenestrules in
the same space measured transversely. In the later and upper
erowth there are three fenestrules only each way in the same
measurements. Cells small, round, their diameter apart, one com-
monly at the end of each dissepiment, and one between, or three
to each fenestrule: this is in the early growth; the later growth
has four in the same space. When the cells occur in the angle
formed by the junction of dissepiment with insterstice, the former
is expanded atthepoint. ‘This feature is not constant. Cell-mouth,
when preserved, nearly on a level with the keel.
Obs. This is a very marked and easily recognized species ; its
square fenestrules and the round-wire-like nature of the interstices
and dissepiments on the reverse face at once distinguish it from all
others. In mature specimens the reverse has a peculiar and
characteristic nodular aspect. Im size it is somewhat minute,
being intermediate between Venestella membranacea, Phil., and
Fenestella plebeca, M‘Coy. Both Phillips and Prof. M‘Coy were
unfortunate in the fragments which they selected for description ;
it is not surprising, therefore, that when a good representative
specimen was found it should be described as a new species.
Hence by far the best description of Fenesiella nodulosa, Phill., is
that given for Fenesiclla bicellulata, R. Ether., jun.
In 1874 Dr. Young and Mr. John Young announced the disco-
very of a new Carboniferous polyzoon, Actinostoma fenestraium, in
which we have all the characters hitherto observed by Phillips, Prof.
M‘Coy, and Mr. R. Etheridge, Jun., in Menestella nodulosa, with the
addition of the cell-aperture terminating in a nipple-shaped pro-
jection, the orifice of which was furnished with eight radiate denti-
cles. To regard Actinostoma as the full development of /. nodulosa
seemed the right course: as such I alluded to it in my former
paper on the Carboniferous Fenestellide. Since then Mr. G. R. Vine,
@ most accurate observer of the paleeozoic polyzoa, informs me that
he has noticed the denticulate cell-aperture in Fenesiella plebaa,
M‘Coy; while recently Mr. John Young, F.G.S., in a paper read
02
184 G. W. SHRUBSOLE—-FURTHER NOTES ON
before the Glasgow Natural-History Society, mentions the occurrence
of the same in Menestella tenuifila, Phill. Thus we have the record
of this peculiar cell-aperture in two if not three species of /enestella.
Notwithstanding this evidence in favour of the denticulate aperture
in Fenestella, I now hesitate to give this feature wholly or in part
to it, since | made the discovery that some of the species of
Glauconome possessed a fenestration not very dissimilar to that of
Fenestella, and might easily, in a fragmentary condition, be mistaken
for it, indeed have been so. ~ There is no doubt about the fact that
some of the species of Glauconome have the denticulate cell-mouth
in question—Gilauconome stellipora, Young, for instance; on the
other hand, it is not equally well established that the cell-mouth of
Fenestella had the same characters. There is the possibility that
some of the fragments of reputed Jenestella upon which the
denticulate aperture was seen, may prove to have belonged to
Glauconome. This discovery of the fenestrate polyzoary in Glau-
conome considerably complicates the question of the nature and
relationship of the palzeozoic Polyzoa; and it will require careful ob-
servation on the part of palxontologists to work out the distinctive
characters of the several genera, and assign to the various species
the right fenestration. The result will have an important bearing
upon Glauconome, more than on Fenestella, since we know so little
of the life-form of the former, whereas the latter is better under-
stood. It may be that both Glauconome and Fenestella and kindred
Polyzoa, possessed the denticulate aperture. It is so far certain,
as regards Glauconome; it may ultimately prove to be true of
Fenestella. But for the present I consider that Glauconome has
absorbed the existing evidence of the peculiar cell-aperture in favour
of its claims. The other problems remain to be worked out.
I will now allude to a connexion which has become apparent
during this inquiry between #’nestella nodulosa, Phill., and Palwo-
coryne, a hydrozoan originally described by Prof. Martin Duncan
and Mr. Jenkins from the Lower Limestone shales of Ayrshire.
With regard to my facilities for observing Palwocoryne, 1 may
remark that it was described * from specimens washed from the
shale, a process necessarily destructive of many of its more
delicate and distinctive features. All the specimens in my posses-
sion, on the contrary, are 7m setw on the shale or limestone in which
they were found. Prof. Duncan, speaking of it, says that ‘“ usually
they are attached by a dactylose pseudo-cellular base to the margins
of the polyzoaria of Henestella’’>. My observations would lead me
to limit the attachment of Paleocoryne to one species of Menestella,
viz. Fenestella nodulosa, and to the pore-face generally, rather than
the margin of the polyzoarium. ‘The frequency with which I
noticed this association of Palwocoryne with Fenestella nodulosa,
led me to go carefully over my collection, and ascertain definitely
the particular species of enestella with which it was most fre-
quently allied. The result was, that, out of ninety-seven specimens
* Hixplan. Sh. 23, Geol. Surv. Scotland, p. 96.
Tt Quart. Journ. Geol. Soc. vol. xxix. p. 413.
THE CARBONIFEROUS FENESTELLIDZA. 185
of Paleocoryne, eighty-five are either attached to the polypite-
face of Fenestella nodulosa or associated with it, while twelve
only are free and unattached. In no one instance is there a sus-
picion that the species is any other than the one mentioned. Simi-
lar evidence to this I get in another way. I have more than one
hundred specimens of /. nodulosa from the shales of Halkin
Mountain, but out of them not one example showing the poriferous
face ; all without exception present to view the reverse side. This
I explain by supposing that, as it is on the poriferous face of Penes-
tella that Palcocoryne finds its seat, that face has in consequence
held the more firmly of the two to the shale. ‘This is really so; for
the base of it may be detected by a slight bulging of the polyzoary
of the enestella, and its presence demonstrated by removing a
portion. There is no similar difficulty in obtaining the obverse
face of the other species from the same beds; nor do the other
species present the appearance on the reverse face which I have
noticed in /’. nodulosa. ‘The concurrence of these two species may
be accidental; but I scarcely think so; the extent of its occurrence
is not in favour of that idea; so that I think we may conclude
that we have good evidence that Palwocoryne in the upper beds of
the Mountain Limestone is exclusively confined to the polyzoary of
Fenestella nodulosa, Phill. I may mention that I have found
Palewocoryne associated with . nodulosa in the middle beds of
the Mountain-Limestone series of North Wales, and also directly
seated upon the poriferous face of the same from the Calciferous
Sandstones of Scotland. I have previously pointed out that several
inferior organisms are parasitic upon or incrust the polyzoaria of /e-
nestella, from Silurian times upwards—such as Hemitrypa, Aulopora,
Alveolites, and Diastopora ; and now Palcocoryne has to be added to
the list. In the case of the previous incrustations there is no doubt
that the parallel branches of the Menestella afforded suitable base-
lines for the attachment of the incrusting coral. Whether there
was any thing more than this in the preference shown by Palwo-
coryne, is one of the problems to be worked out; and it will, IL
have no doubt, receive due attention at the hands of Prof. Martin
Duncan, to whom I have handed over my specimens of Palcocoryne
for further elucidation.
FENESTELLA PoLYPORATA, Phill. Geol. Yorks. pl. 1. figs. 19, 20.
Fenestella multiporata, M‘Coy, Syn. Carb. Foss. Ivel. pl. xxvii.
fig. 9.
intermedia, Prout, Trans. Acad. St. Louis, p. 231.
variabilis, Prout, Trans. Acad. St. Louis. p. 231.
Sp. char.—Polyzoarium foliaceous at first, arising from a stem,
ultimately becoming a flat circular network. Jnterstices large,
broad, rounded, keeled. Dissepiments thin, one third the thick-
ness of the interstice, somewhat irregularly placed, not expanding
at junction with interstice. enestrules large and elongated, three
times as long as wide. Four fenestrules in the space of two lines
186 G. W. SHRUBSOLE—FURTHER NOTES ON
measured transversely, and two fenestrules in the space of two lines
longitudinally. cel rounded and well developed, marked along its
course with numerous spiny processes. ores small and round,
their own diameter apart, prominent when preserved, from five to
nine in the length of a fenestrule.
Obs. This is the largest species of Carboniferous Lenestella, as
regards the size of its interstice and fenestrules, although not so as
to the ultimate growth of its polyzoary, which is considerably less
than that of F. plebea, M‘Coy. This peculiarity at once dis-
tinguishes it from any other species. It is subject to considerable
variation, and will be met with both larger and smaller than the
one described. Prof. M‘Coy, in his arrangement of the Fenestelle,
assigned the smaller type to Phillips’s /. polyporata, and the type
with the larger development and greater number of pores he de-
scribed as I”. multiporata; but as both conform so well to the type in
other respects, there is no reason for this division. This species
often, on the reverse, attains to the size and character of some of the
Polypore, from which it may readily be known by having only a
double row of pore-cells.
Lenestella polyporata never occurs very freely in any locality, but
seems generally distributed throughout the Carboniferous strata.
FryEsrecta crassa, M‘Coy, Syn. Carb. Foss. Irel. pl. xxix. fig. 1.
Fenestella laxa, Phill. Geol. Yorks. pl. 1. figs. 26-30.
My previous notice of this species was limited to the extent of
showing the identity in character between the species respectively
described by Phillips and Prof. M‘Coy as VFenestella laxa and
Fenestella crassa. Since then a wider acquaintance with the Car-
boniferous Polyzoa, and more especially with the Irish species in my
possession, has caused me to hesitate about including it among the
Fenestelle, since I have good reason for believing that the frag-
ment which has been described as such will be ultimately found
to belong to another fenestrate genus of Polyzoa. The original
drawing of this species by Phillips clearly included two species of
Polyzoa—one a Polypora with three rows, and the other apparently
a Henestella with two rows of pores—the latter from Ireland, be it
remembered, where in certain localities Jchthyorhachis Newenhamu,
M‘Coy, and Glauconome grandis, M‘Coy, are not uncommon.
Specimens in my possession lead me to say that I have little
doubt of being able to show that the fenestrated form described as
Frenestella crassa, M‘Coy, is likely to prove to be the network or
polyzoary of one or other of the above species, or some kindred
form.
A glance at the drawings of Fenestella crassa given by Prof. M‘Coy
would seem to confirm this view. The coarseness of the interstice,
and irregularity of the dissepiment and growth generally, are not
characteristic of the Fenestellide. Its true affinities have yet to be
ascertained. or the present it is enough to say that its claims to
be considered a Fenestella are very doubtful.
THE CARBONIFEROUS FENESTELLID ZA. 187
FrnESTELLA HALKINENSIS, Sp. Nov.
Sp. char.—Polyzoarium a flat, oval, or circular expansion, folia-
ceous in its early growth, having a stem and expanded root-base.
Interstices flat, broad, very slightly rounded, keeled, the sides often
showing a flap or fringe. Dissepiments irregularly placed, very
thin in early stage, gradually thickening, rarely more than one
third of the thickness of the interstice. enestrules elongated,
becoming oval with increased growth, four in the space of two lines
measured longitudinally, and six in the same space transversely.
Pores small, round, often twice their diameter apart, three in the
length of a fenestrule, four and sometimes five in the later and
larger growth. cel a narrow round wavy line, having three
nodes in the length of a fenestrule.
This species at first sight would seem to have a strong resem-
blance to Fenestella plebeia, which, however, is soon dispelled by
careful scrutiny ; for it will be found to possess scarcely a feature
incommon. Its broad flat interstices at once distinguish it from
the round or more often angular stem of J”. plebera ; while the greater
distance between the cell-pores, and the thread-lke nature of the
keel, complete the distinction. Again, the growth of /. plebeva is
noticeable for its regularity and smoothness, while 7. halkiensis is
by comparison coarse and irregular. The root-base of F. plebeia is
secured in position by numerous rootlets; while /. halkinensis has
a broad, expansive and adherent base, which is further strengthened
by the interstices which, in favourable positions, directly adhere to
the rock by a similar flat calcareous base. Its expansion was not only
much smaller in size than that of F. plebeia, but the last details would
seem to indicate a species of dissimilar habits, by attaching itself
to rock-surfaces which the rootlets of /. plebeia would fail to enter.
The affinities of this new species are, on the other hand, clearly with
Fenestella polyporata, Phill., rather than with F. plebeia. It has
very much the appearance of being a diminutive variety of enes-
tella polyporata, especially on the obverse face.
Locality. Fairly abundant in the Cement-stone Quarries near Pen
yr Wylfa, Halkin Mountain, North Wales.
It will be noticed that I have described only five species of
Carboniferous Fenestelle. I by no means wish it to be understood
that I do not believe in the existence of species other than those I
have described. Of these F. plebeia, M‘Coy, F. nodulosa, Phill.,
F, polyporata, Phill., and F. membranacea, Phill., are really the
principal and prevailing forms, and will be found in more or less
abundance in association with other Polyzoa, from the Calciferous
Sandstones of Scotland to the topmost beds of the Mountain-
Limestone series of North Wales and elsewhere. The only partial
exception to the rule is Fenestella membranacea, Phill., which is
either absent or not so abundant at certain points and localities.
Having proved the existence and association of these species at
various horizons in the Carboniferous series, I speak confidently as
to the fact that the leading species of the Carboniferous Fenestelle
are few in number, while the reputed species are made up from the
188 G. W. SHRUBSOLE—FURTHER NOTES ON
mutilated and altered fragments of the polyzoarium in all stages of
its growth, not only of Fenestella, but of Ptylopora, Glauconome,
and Ichihyorhachis, all of which presented a reticulated character,
which under certain conditions might have been (and, indeed, has
been) mistaken for that of Fenestella. Hitherto it has been the practice
to assign any free fenestrate fragment of a polyzoan to Wenestella.
With the discovery to which I have alluded, that Fenesteila was not
singular in possessing a fenestrate polyzoary, the error of that
method of determining polyzoan fragments becomes apparent.
The few species to which I have reduced the British Carboniferous
Fenestellide is, I find, in perfect. agreement with the results arrived
at on the American continent. Prout has published * a list of eight
species of /enestella from the Carboniferous rocks of North America ;
although no plates are given, the details of the species are so minute
as to leave nothing to be desired in the way of description. Of
these eight species there is only one (Lenesiella Norwoodiana) that
has any claim to be considered a new species ; they correspond exactly
with the types of our various English species. Prout did his work
without the aid of Prof. M‘Coy’s book on the Carboniferous Fossils
of Ireland, in which the Fenestellide are for the first time
adequately described. The result of Prout’s independent research,
apparently with ample material, is that only five good species are
made out. These American synonyms I have placed for the first
time under their respective English species.
There are possibly a local species or two of Fenestella which I
have not described. Ltnestella halkinensis is one of these local
forms. I have not met with it elsewhere than at Halkin Mountain.
These local species require to be very carefully worked out before
they can be definitely pronounced to belong to the Fenestellide. I
would suggest, with a view to the prevention of a needless mul-
tiplication of species of Fenestella in the future, that, before descri-
bing a new species, the nature of the attachment of the fenestration
should be definitely ascertained, whether to a root-stalk with root-
lets, as in Fenestella, or to a midrib or stem, as in Péylopora and
Glauconome. Nor do I consider this standard too high. I have
adopted it with the five species which I have described. Owing to
the complicated surroundings which I have shown to be connected
with Henestella and the forms allied to it, I am strongly of opinion
that some such course of procedure is necessary.
The following table of the measurements of the leading features in
the several Fenestelle will be found of considerable service in es-
tablishing their identity.
* Trans. Acad. St. Louis, vol. i. p. 228-286.
THE CARBONIFEROUS FENESTELLIDA, 189
N ie
NT | Number
ne mee of fenes- | of fenes-
aaa gees aren Shape of | trulesin. | trules in
co Lissep;. | fenestrule.| two lines | two lines |
Seer : trans- | longitu-
; versely. | dinally.
|
| Fenestella plebeia, M‘Ooy..., 3-4 Oval. 6 ce
membranacea, Phill...., 3-4 Opreng, 8 | :
nodulosa, Phill.......... | 3-4 | Square. | 6-8 noes
polyporata, Pile 6-9") | | Elongate. 4 | 2
halkinensis, Shrubsole| 3-4 | Elongate. | 6 ay 4 |
Discussion.
The Presrpent stated that this group, which ranged from the
Llandeilo to the Permian, is often represented by very imperfect
specimens, and that there is great difficulty in discriminating the
forms. Nowhere are they so well preserved as in the Carboniferous
rocks of Flintshire and Scotland.
Dr. Mucrre spoke of the value of the method adopted by the
author in studying the varieties of growth and development in each
species.
Prof. Snetey regarded the principle on which the author had
worked as a very sound one, and he thought that such revisions of
certain life-groups were calculated to be of the greatest service to
geology.
The PrestpentT remarked upon the difliculty that arises from the
fact that many type specimens are inaccessible for reference. He
deprecated the creation of new specific names before a rigid com-
parison had been made with the old ones.
190 PROF. P. M. DUNCAN ON THE
14. On the Corarttirerovs Suriss of Srnp, and ets Connexion with
the last Upuuavat of the Himatayas. By Prof. P. Marty
Duncan, M.B. Lond., F.R.S., F.L.8., &. (Read February 2,
1881.)
ConrTENTS.
I. Introduction: the History of the Geology of Sind; Questions involved.
II. The Stratigraphical Position of the Series and of the Ossiferous Manchhar
deposits.
III. General Results regarding the Alliances and Peculiarities of the Corals of
the Series. The Prenummulitic, Nummulitic, Oligocene, and Miocene
Coral-faunas of Sind.
IV. The Equivalence of the Mancbhar and Sivalik deposits.
V. General Considerations regarding the Age of the last Himalayan Uplift.
I. Introduction §e.
A memoir by Grant, illustrated by Sowerby, which appeared in the
‘Transactions’ of the Geological Society (series 2, vol: v. 1837), first
brought the countries west and east of the Indus under the notice
of European geologists. Fossils from Sind, Baluchistan, and Cutch
were therein described ; and the types were presented to the Society.
But it is to Mr. Vicary that science owes the first attempt at a com-
plete description of the geology of Sind*. Written in 1847, the
fossils which should have illustrated his paper, and some others
collected by Lieut. Blagrove in Cutch, were handed over to
MM. d’Archiac and Jules Haime for examination and publica-
tion. Their fine work, the ‘ Description des Animaux Fossiles du
groupe Nummulitique de Inde, was published in 1852. They only
recognized one geological horizon, the Nummulitic, although Grant
had expressed an opinion that there was more than one fossili- —
ferous series. Messrs. Cook and Carter added to the knowledge of
the Baluchistan area in 1860; and the last-named naturalist felt
it necessary to give a Miocene age to some fossils which Sowerby
had figured for Grant. On the other hand, MM. d’Archiac and
Jules Haime severely criticised M. d’Orbigny for stating that some
of their Sindian species were of Falunian age, and decided against
Dr. Carter’s grouping of some of the marine Tertiary beds as
Miocene x.
In 1863 Mr. Henry M. Jenkins, F.G.S., at that time Assistant-
Secretary of this Society, and myself were endeavouring to learn
something about Tertiary deposits situated as remotely as possible
from European types.
A collection of Mollusca and Corals from Java had been sent to
the Society by M. de Groot; and we proceeded to examine them;
and in order to determine the affinities of some, which seemed to be of
younger age than the Nummulitic, it became necessary to study the
work of MM.d’Archiac and Haime on India and to examine their types.
We found that there was a species in Java which my friend called
* Quart. Journ. Geol. Soc. 1847, vol. ui. p. 334.
t Cook, Trans. Med. Phys. Soc. Bombay, vol. vi. pp. 1-45; Carter, Journ.
Lombay Royal Asiatic Society, vol. vi. p. 184.
t See Carter, Geol. Papers on Western India, pp. 628-776, and the general
résumé in their work already noticed.
CORALLIFEROUS SERIES OF SIND. 191
Vicarye callosa, and that it was closely allied (the distinctions being
only of ornament) to Vicarya Vernewlit, D’Arch., from Sind.
This Vicarya of Java was associated with species which are closely
allied to those of the Miocene of Western and Eastern Kurope.
A Coral (Heliastrea Herklotzi, Dunc.) from Java resembled the
Miocene Heliastreeans more than those of the Kocene*.
Following up the subject carefully, 1 examined all the collections
submitted to MM. d’Archiac and Jules Haime; and to my surprise I
found that they had neglected many specimens which had not only
a Miocene but even a Pliocene facies. The identity of some species
with members of the West-Indian Miocene Coral-fauna was tolerably
evident; and whilst admitting the similarity of the mineral con-
dition of all the fossils, I divided the genera into those which else-
where are found in Hocene, Miocene, and Pliocene formations.
During the following yeart I examined and described twenty-
six species of Corals from Sind, from unknown geological horizons
near Karachi. Some had been previously described by D’Archiac
and Haime; but the bulk had not. ‘he evidence of the existence of
three Tertiary deposits instead of one seemed overwhelming.
Subsequently the Geological Surveyors of India, Mr. W. T.
Blaniord, F.R.S., and Mr. Fedden, made an elaborate survey of
Upper and Lower Sind, and Messrs. Wynne and Fedden of Cutch.:
In the last-mentioned district fossils were found which proved
the equivalency of the deposits with those of Sind, and that there
was a higher Tertiary horizon than the Nummulitic.
The Corals collected in Sind by the Survey, under the superinten-
dence of Messrs. Blanford and Fedden, and carefully marked with
figures denoting their geological horizons, were sent to me by Mr.
Medlicott, F.R.S., the present Superintendent of the Survey, so that
they might be described in a volume of the ‘ Paleeontologia Indica.’
But simple description was not all the requirement of the Survey
and myself. Certain questions of great importance had arisen in
the geolcgy of India; and it was probable that the determination of
the age of the coralliferous strata would assist in deciding the ages
of the Himalayan upheaval, of the Sivdlik deposits, and of certain
olive shales underlying a trap at the base of the Nummulitic series—
questions which had been attempted and had been answered by
Messrs. Medlicott, Blanford, and Lydekker, and which required
some confirmatory evidence.
There was another reason why I should be honoured by the Geo-
logical Survey of India asking me to undertake the description of
their splendid collection of fossil Corals from Sind. In my Presi-
dential Address for the year 1878 I criticised the opinions of my
friends Messrs. Medlicott and Blanford regarding the age of the
Himalayas, and inferred that their decision regarding the Post-
pliocene date of the so-called Nerbudda fauna, was influenced by
the discovery of a human implement in the containing deposit.
They took the very philosophical course of affording me the means
of converting myself to their opinions.
* Quart. Journ. Geol. Soe. vol. xx. p. 45.
t Ann. & Mag. Nat. Hist., April 1864 (Fossil Corals from Sind).
192 PROF, P. M. DUNCAN ON THE
J
The description of the Corals has been published in a volume of
the ‘ Paleontologia Indica ;’ and although the evidence regarding a
Pliocene marine fauna failed, there is no doubt about the former ex-
istence of Lower and Middle Tertiary coralliferous deposits in Sind.
Il. The Stratigraphical Position of the Series and of the Ossiferous
Manchhar Deposits.
The detailed description of the geology of Western Sind is to be
found in the Memoirs of the Geological Survey of India, vol. xvii.
part 1 (1879), by W. T. Blanford, F.R.S. &e., Deputy Superintendent
of the Geological Survey of India; andit is therefore only necessary -
to explain those parts of it which relate to the general succession of the
stratigraphical series and the position of the strata yielding Corals.
The mountain-ranges west of the Indus run nearly north and
south, in irregular parallel series. The longest range, the Khirthar,
is slightly curved, the concavity being to the east; and it extends
from slightly south of 26° N. lat. to close to 28° N. lat. The Laki
range, more to the east, is nearly coincident with the sixty-eighth
parallel of east longitude, and extends from the Indus north of
26° N. lat. to nearly a degree to the south. Other minor but
nearly north-and-south ranges occur; and the whole were com-
prised by MM. d’Archiac and Haime under the title of the Hala
range (a name unknown to the natives).
The following is the list of geological formations in Western
Sind, and which are to be recognized in one or other of the moun-
tain-ranges * :—
| amantell |
Group. Subdivisions. pe Age. Remarks.
feet.
ALYUN EA RG oe |eae eeleneeeene ? Post-Tertiary.
i (Uipperyic sce OOO shacsonae Plioceneteeee Unfossiliferous.
MESSCHEAB 00. { mae eno 3000-5000 ...| Old Pliocene or} Vertebrate remains.
Upper Miocene.
GAS PRR SEER WDC ER RE at 1000-1500 ...| Miocene ............ Coralliferous; no
Nummulites.
| Wiper meeeeacs 4000-6000 | scl brad epee eee Unfossiliferous.
NARI wecrccree Oligocene. ( Coralliferous, with
| Tower:.......: 100-1500 | VaR ile nnn game Nummulites garan-
Sensis.
{ Wipperyeeees.: 500-3000...| Nummulitic ...... Nummulitie lime-
KHIRTHAR .. stone.
I OWers acces GOOO'? a..36 sacle erence Unfossiliferous.
IRANIKOT cuca digester cee D000 eae Lower Nummu-| Fossiliferous.
litic. Corals and Nummu-
lites.
RAP ys so AO | gr Mea Rr Cana AD-90 ewesea oe Decean Trap.
(| Cardita Beau-\ 350-450 ...... Transition beds ...| Fossiliferous.
|| sandstones ..| 700 © Hori t det
andstonesi.|) (OO meesccnecs si. retaceous. orizon not deter-
ee racrous 1 Limestones | 320. mined.
|| with Hip-
(| purites.
* From the Memoir by Blanford, p. 32, slightly modified.
CORALLIFEROUS SERIES OF SIND. 193
Explanatory Sections.—In the Laki range, south-west of Amri
on the Indus, are dark-coloured hills which contrast with the cliffs
of grey and white Nummulitic limestone behind them. A section
close to the hill called Barrah is given by W. T. Blanford, F.R.S. ;
and it shows that the range consists of three parallel ridges (see fig. 1,
p- 194).
The outer, to the east, is composed of Tertiary rocks, while the
intermediate one consists of Cretaceous beds faulted to the eastward
against the Lower Eocene strata, and dipping under them io the
westward.
This section shows the normal sequence of the groups of strata
from the Cretaceous to the Khirthar inclusive. Above the Nummu-
litic limestone of this last group the Nari and Gaj series are wanting,
and the Manchhar succeeds*.
On the Gaj river, in the Khirthar range, W. T. Blanford remarks
that a thickness of at least 25,000 feet of strata is exposed (see
fig. 2,p.194). The succession from west to east 1s :—unfossiliferous
strata, probably of Cretaceous age, followed by Khirthar strata (the
Ranikot series, the lowest Eocene, being absent); then the lower
and upper Nari series come in, and are followed by the Gaj and
the Manchhar deposits.
The lowest coralliferous deposits occur in the soft olive shales and
sandstones with volcanic ash, belonging to the Cardita Beaumonti
Series below the trap. The accompanying remains are those of
Amphiccelian Crocodilia and Echinodermata; and the deposit was
neither a reef-structure nor a deep-water one.
The lower part of the Ranikot series, resting immediately on the
trap, consists of soft sandstones, shales, clays with gypsum and lignite,
and pyritous shale. A few fragments of bones and some dicoty-
ledonous leaves occur. ‘These freshwater strata are succeeded by
highly fossiliferous marine limestones, often brown in colour, inter-
stratified with sandstones, shales, clays, and ferruginous bands.
Nummulites appear for the first time, and there is a grand develop-
ment of Corals, Echinodermata, Gasteropoda, and Cephalopoda. It
was not a very deep-water formation. Hrosion of the surface of the
Ranikot strata occurred before the deposition of the next series.
The Khirthar series includes in its highest portion a massive, pale
or dark grey, hard, compact Nummulitic limestone whose extreme
thickness is 3000 feet. It thins out to the south-west, and disap-
pears within a distance of twenty-five miles of its greatest develop-
ment. Other Nummulitic limestone-beds are found, which may be
lower in the series ; and they and the main group are represented
elsewhere by shaly limestones and sandstones with calcareous bands.
In some districts flint occurs in a limestone with Alveolinw. The
lower members of the series are often wanting, and are well repre-
sented by shales, marls, and sandstones and where these are present ;
unconformity with the underlying .Ranikot beds is not seen; but
where they are absent the Nummulitic limestone (as in the Laki
range) rests unconformably. The compact limestone is of course
x Memoirs Geol, Survey of India, vol. xvii. pt. 1, p. 151.
PROF. P. M. DUNCAN ON THE
194.
)
——
WENT ToMOT Sf pus ‘xeddn ‘9 {fey ‘p ‘savyYouepy comoy ‘9 ‘soddn ‘9 fureyd snpuy ‘»
*IVYYOuB ‘Teo "118 NT . *TVY JALIL "s00084019
—_— A eee 1 oe creme con neers eee recess SN ee SE SS re Q---— 4
oI
Se
Rane
eee ane
wee wee ee
ee---— —-—
snpuy “gH eney9 “rey ANIL
(ozis yey “proyurrg 104zV)
‘ony (ny ayy fo yung yptou ayn v0 ohuny mypnyy fo woyoay onoumunibyrp [n.10U09—% *S1 yf
‘g ‘oUOJSOTUT] AVYZATY, OYJ pur ‘ssouyoryy yvoasd Jo st yor ‘9 ‘dnosd yoyravy
ey} wsy} pure ‘sMor[oy ‘p ‘deay oyy, ‘a “yuownvog vpplnD YIM SeTLYS OATTO oA’ STIL OT} Jo ysoAA ‘sovoq ueTIYdoa ATyuoIvdde
jo syuoutseay pure stoysho SuLureyUOD poq ¥v st STII oY Jo doz oy} UG ‘ST[TY pecmopoo-yavp oyy Jo doz oT surtoy tf ‘soulojspuLs Jo
SSOUWOIY] yvors YW ‘sopranddizy sureyuoco pur [IPT Yyerawg oy} Jo osuq oy} sumtoj ‘/ ‘ouoysouny, sip, “yuri v suroq Arwpunog oyy
‘ouojsoutty Aors puv oy Jo ype gsurese Apdnaqe puso soyy, ‘crip pestoAod v ITM osye “no do.to ‘9 ‘dnoas yoyrury, oy] JO saoquIEut
aaddn oy} yor ut ‘punoas MoT oUTOS st OSPIA OY} JO JSoAA ‘OSPIA Wtoysva OY} SUIAOJ oUOJseETMUTT STT, “480A\ oY} 0} Sutddrp speq ouy
‘9 ‘oUOYSOUTT] ONTNWUINA AvyyAIYYy UO UeY} pue “Va2vawharTy sapynuwun\y YA ‘ose avqzaIyyZ Jo sAvypo oped uo ysou “VyvaysS TeTOULTL “#
PARE. e
W SA RSS| <=,
Is VG}
TS |!
ee
Ne
qm “TE Were
(4903 QOGY 0} Your T ‘epeog) “W2FT young ybnowy, WOLVIG—'T *SLy
|
1
{
hs
i
|
‘
“4923 006T TINH ang “HOATE [B) 293 000 “JooF Q00e “wear [vQ ‘YB
“AA
CORALLIFEROUS SERIES OF SIND. 195
highly fossiliferous ; but it has not yielded very good specimens of
Corals. The indications of a fringing-reef-building fauna, or a bank
of coral, are distinct; but the species when compared with their
modern analogues do not indicate a great reef-development.
Amongst other fossils, Lamellibranchiata prevail, and the Echini are
numerous; but the Nummulites and Orbitolites, Alveoline, and
Patelline are the most important organic remains. Amongst the
Nummulites there are WV. Ramondi, N. biaritzensis, N. Beaumonin,
NV. granulosus, and N. Leymerier.
The Nari series rests conformably on the Khirthars; and there is
occasionally an apparent passage from the Khirthar limestone into a
yellow or brown rock of the Nari group. There is, however, a
biological break; for the Nummulites of the upper group are
characteristic, and differ from those of the lower. The Khirthar
forms are not found, and Nummulites garansensis appears with Orbi-
toides papyracea, in the Nari series. The rock is a limestone with
intercalations of sandstones and shales. Asa rule, shales, fine sand-
stones, and occasional bands of limestone form the base of the Nari
group, and pass upwards into coarse, massive, thick-bedded sand-
stones, attaining a thickness of from 4000 to 5000 feet on the eastern
flank of the Khirthar range.
A local break occurs to the south, and the Upper Nari beds rest
unconformably on the denuded edges of the Lower Nari brown
limestones; and still further south, fifty miles east of Karachi, there
is a well-marked distinction between the upper members of the
group with Orbitoides papyracea and the lower with Nummulites
garansensis; and in one locality the upper member overlaps the
lower, and rests on Khirthar limestone.
To the east of the Laki range the Nari beds are wanting, and the
Mancbhar series rests unconformably on the Khirthar, with some
pebble-beds of the Gaj series intervening. But to the west of the
range the Nari and the Gaj series are found in their normal sequence ;
and towards the coast the exact distinction which can be drawn
elsewhere, stratigraphically and petrologically, between the Ter-
tiary series is not possible: this is mainly due to the disappear-
ance of the limestone element of the Khirthar and Nari series, and
to the prevalence of sandstones and shales. The fossils, however,
distinguish the groups: but the horizons of the zones of Nummu-
lites and Orbitoides vary, being higher or lower in their proper series
according to locality.
The upper sandstones of the Nari group have not yielded marine
fossils, and in Upper Sind they contain the remains of plants.
The Nummulites become fewer in their species at the base of the
Nari group, and cease to be found in the lower beds of the suc-
ceeding series, the Gaj.
The Gaj group, with a base of highly fossiliferous limestones and
calcareous beds, more or less shaly and stratified, overlies the softer
shales and sandstones of the Nari series. The development of the
calcareous series is great; but it is subordinate to an arenaceous
element. ‘The sandstones are intercalated with clays with gypsum;
196 PROF, P. M. DUNCAN ON THE
and shales and bands of limestone, highly coralliferous, are very
constant.
The Gj series rests conformably on the Nari series; although
there is a mineralogical break, the passage is so oradual that cu
careous bands of the Gaj series are found interstratified with the
uppermost Nari sandstone. The Gaj series overlaps the Nari to the
south and rests on the Khirthars, and is wanting in Lower Sind to
the eastward of the Laki range
North-east of Karachi the series is highly developed, and massive
limestones occur ; they reach as far as the coast.
The uppermost beds of the Guaj series are variegated clays and
grey sandstones, which form a passage into the everlymg Manchhar
strata, and contain species of Ostrea, Corbula, Arca, Scalaria,
Buccmum, and Turritella. A crab of the genus Typilobus and the
Vicarya Vernewliw already noticed have also been found there.
The oyster is like Ostrea multicostata. 'The Echinoderms are of the
genera Maretia, Meoma, Breynia, Clypeaster, &e. The Corals found,
principally associated with the lmestone-beds, are very different in
their aspect from those of the underlying Nari group. They belong
for the most part to reef-building genera, and some are represented
in modern reefs by allied species, which grow in the surf and in the
most exposed parts. ‘The rest were dwellers ; in quiet water. Great
masses of the coral limestone consist of Stephanocena maxima in
casts, and the presence of the genera Madrepora, Hahastrea, and
Porities is very significant of s shallow-water conditions.
Resting on the Gaj strata is the Manchhar group; and where the
Gaj beds are wanting, and even where the Nari series is deficient,
this upper group rests on the Khirthars.
Of ereat thickness (10,000 feet on the flanks of the Khirthar range)
the Manchhar series is divisible into an upper and a lower group. In
the lower group much grey sandstone, soft and fine-grained, and
composed of quartz with some felspar and hornblende, is found ; and
red sandstones and conglomeratic beds exist towards the base, as
well as red, brown, and grey clays. The conglomerates do not
contain pebbles of older Tertiary rocks; but cream-coloured clay,
soft sandstone, quartzite, and micaceous shale are found in them.
The conglomerates near the base are ossiferous; and the vertebrate
remains are teeth or bones more or less rolled. There is no satis-
factory distinction to be made on the Gaj river between the estua-
rine beds at the top of the Gilj series a the lowest beds of the
Manchhar; and osseous remains have been found in the upper Gaj
series.
The upper part of the Manchhars has a conglomerate in it with
stones derived from the older tertiaries ; below it are red, brown, or
buff sandstones, with some clays; and there ure no fossils.
Although usually conformable to the Gaj series, in places the
Manchhars rest on the older rocks ; ; and there are proofs of the Gaj
strata having been greatly denuded before the deposition of the
Manchhars.
In the Laki range the Manchhars have an ossiferous conglo-
CORALLIFEROUS SER1ES OF SIND. 197
merate near the base. In the Vero plain, running southward along
the eastern side of the Laki range, south of Ranikot, large frag-
ments of silicified wood are common, and some trunks of trees are
upwards of 30 feet in length and 10 in girth. In the south, near
Karachi, the Manchhars pass into Gaj strata, and marine fossils are
associated with the lowest beds.
The general conformity of this great tertiary series is evident—
although local unconformities occur, and there is evidence ‘in
fayour of there having been some disturbance of the older rocks
before the deposition of the Lower Manchhar group. The sub-
sidence which took place during the deposition of these thick shallow-
water deposits was vast; and there were occasional slight upheavals.
The final epoch of the mountain-formation occurred after the depo-
sition of the Manchhars. The strike of the chains is in the main
north and south; and the thrust came from the west to the east, and
from east to west.
The date of the grand mountain-formation is subsequent to the
deposition of the sedimentary strata forming the Upper Manchhars.
III. General Results of the Study of the Corals of the Series.
The Corals of the strata with Cardita Beaumonti below the trap.
are shallow-water forms; and their development indicates conditions
untavourable to vigorous coral-growth. There was no reef. The
species are new ; and there are no characteristic Cretaceous or Hocene
forms present. The Smelotroch: and the Lhabdophyllic are Secondary
genera; but the first-named had species inthe European Tertiaries, and:
may be represented in the shallow seas of the present day. The Cary-
ophyllice of the deposit have four cycles of septa only ; and this gives.
them somewhat an ancient look ; and the Litharwa would pass either
as a Cretaceous or as an Eocene form.
The fauna as a whole is deficient in characteristic forms, and may
be considered transitional.
It has been stated by the Geological Surveyors that the trap re-
sembles the Deccan and Malwa trap; and the position of that vast
outburst is anterior to the Nummulitic age, and subsequent to some
Cretaceous strata in Western Central India. Certainly there are no-
Nummulites in the sands and shales which contain the fessils; and
these are the remains of a Cretaceous crustacean.
The Corals of the Ranikot group are numerous in genera and
species ; and the fauna is remarkable for the number of simple forms:
it contains, and for the predominance of the family Fungide.
The compound Corals of the family Astraide, which so largely
enter and have entered into the composition of reefs, are but feebly
represented ; and the few species which have been described did not
ageregate to form massive limestones, but were seated on small flat
circular epithecate bases. Fine as were many of the growths, yet
it was a stunted Coral-fauna; and the shape of the majority of the
forms would rather indicate that they lived in still water, and not
in the rush of the waves. Certainly the Corals were beyond the
Q.J.G.8. No. 146. P
198 PROF. P. M. DUNCAN ON THE
rolling or scouring action of the sea; for any such movement would
have displaced most of them.
As a generic assemblage, the Ranikot Corals are Kocene in facies;
and of the twenty-seven genera three are new, and oneis known in the
Miocene of the West Indies. Out of fifty species seven are identical
with European Eocene types, which are not found, however, as a
whole, on one geological horizon in Europe. Some of them are
found in the Lower Eocene; and the others are to be noticed in the
deposits of San Giovanni Ilarione and of the Oberburg, in Styria, and
in the higher horizon of Castel Gomberto. These forms are located
in one series in Sind, and at the bottom of the Nummulitic group.
Five species are closely allied to Kuropean forms out of the same great
vertical series; and about seven others have a distinctly European
facies. These 19 species give the Eocene charaeter to the fauna.
The most distinctive genera are Stylocwinia, Plocophyllia, Stepha-
nophyllia, Stephanocenia, Prronastrea, Reussastreea, Cyclolites, and
Litharea. It is remarkable that five well-marked species of the
genus Turbinoseris (nobis) should have lived on the Indian area;
they are allied to those of the Eocene of St. Bartholomew in the
West Indies.* ‘The genus is Lower Cretaceous in England ; and, under
another name, it has lately been introduced into the N attheim
oolitic Coral- fauna.
The presence of a species of St yline and of Thamnastrea recalls
the Jurassic and Cretaceous ages: ‘the first is found also in the next
or Khirthar series of deposits; and'thé last probably lived longer in
the southern seas. Only one genus, Placocyathus, is a Miocene type ;
and its distribution is West-Indian.
There is one very remarkable species, Stylocenia maxima, nobis,
in the Ranikot group; and it is so called from the great size of the
intercalicular projections, which are little monticules in the British
Stylocenia emarciata, Lamk. sp. ae emeniun of the Cages base
of the coral is 3} inches; an A
concentric epitheca is on the base; and the upper surface i is @ mass
of calices, and tall columns between them, some reaching 75 inch in
height. The minute columns in the British | ‘species are proved by
the examination of these gigantic growths to be stunted or aborted
calices. Some of the processes of Btylocoenia maxima have a perfect
calice on the top, and the costs come down the side; others have ill-
developed calices, and a mere representation of a columella and septa.
It is acommon form, and is characteristic of ‘the Ranikot series;
its nearest ally is Stylocania macrostyla, Reuss, which is associated
with Nummultes planulatus and Cerithium ¢ Uh iganteum in the district
of San Giovanni ilarione.
Young specimens, of course, greatly resemble the European Stylo-
coenia emarciata of Bracklesham age.
‘Two other species of Stylocoenia are very common: one, S. Vecaryt,
was described by D’Archiac and Haime ; and the other is new. It has
a large circular epithecate base ; and the calices are large.
Astr ocoenta, that very widely distributed genus, whose range, ver-
* P. M. Duncan, Quart. Journ. Geol. Soc. vol. xxix. p. 554,
CORALLIFEROUS SERIES OF SIND. 199
tical and horizontal, is enormous, has several species in the Ranikot
eroup: and Astrocenia ramosa, Sowerby, a Cretaceous type from the
Turonian of Gosau, found also in the Hocene of St. Bartholomew
in the West Indies, is present in Sind, and has the usual tuberose
branchlets so characteristic of the form.
Large solitary Corals of the genus Montliwvaltia abound, and also
a characteristic series of simple forms which I have had the oppor-
tunity of naming after Mr. Fedden, to whom the geology of Sind
owes so much. The genus Meddenia had its young forms growing
on small shells, which, with the growth of the base of the Coral,
were enclosed, and the Coral became free. This is not an unusual
habit in some two or three species of Corals of another family,
now living; and an elongate base is produced. One of the
results of this change of condition was that the coste did not
radiate upwards from the peduncle, as is seen in the larger forms,
but from the whole length of the enclosing base. Another pecu-
harity is that the epitheca is like a broken mosaic.
There are three well-marked species of this genus; and one has
two good varieties in the Ranikot series. It is near Montlivaltia as
a genus; and, admitting the great variability of all simple or
solitary Corals, it is very possible that the unusual method of
early growth may have produced correlative changes in the general
shape and septal arrangement. The genus was restricted to this
Lower Eocene horizon. Amongst the great series of Fungide found
in the Ranikot group there are two European forms of Cyclolites ;
and the other seven species of the genus are well differentiated.
Finally, the genus Stephanophylliia, amongst the Kupsammines,
ought to be represented, to give the full early Tertiary facies to
the Cyclolitic assemblage. Stephanophylla indica, from Jhirk, in
the Ranikot group, maintains the character of the genus for beauty,
and is an exquisite gem. Its affinities are rather with the Cre-
taceous species; and it differs but slightly from S. Bowerbanki of
the Lower Chalk in its main characters, and from S. discoides of
the London Clay more decidedly. Like most of the Ranikot corals,
the individuals of the new species began life by settling down on a ~
Nummulite; this formed the permanent base of the coral; and the
usual radiating costal arrangement of Stephanophylha either does
not exist or cannot be seen for the Nummulite.
Khirthar Serives.—Sixteen species of Corals were found in this
series; but ten of them were taken from beds so high up that it
is not satisfactorily proved whether they are at the top of the
Khirthars, or form the base of the Nari group, next in vertical
succession. By separating these ten species, an indubitable
Lower-Khirthar fauna is decided to have existed: its biological
conditions were unfavourable to vigorous coral-growth ; and there
were no littoral or reef-building forms. From the analogy of
recent forms, which are identical generically with those of the
Khirthar series, or whose shape resembles that of the ancient species,
a sea-floor at the depth of from 20 to 200 fathoms or more would
be indicated.
RP 2
200 PROF. P. M. DUNCAN ON THE
The species belong to the genera TZ'rochocyathus, Leptocyathus,
Stylophora, Montlivaliia, Calamophyllia, and Astrocema. The
Trochocyathus is one of the discoid group, and the Leptocyathus is
of course a low flat Coral. The Stylophora is a minute Coral; and
so is the Astrocenia. But the Montlvaliia is a finely grown form ;
and so is the Calamophyllia. Of these, Stylophora contorta,
Leymerie, has also been found in the Kocene of the West indies and
at La Palareain Europe; and Astrocenia nunusma, Defrance, sp., is
a Nummulitic form at Gap, in the district of Nice. This little
assemblage is thus clearly of Hocene age. No distinction can be
made between this and the preceding deposit, as regards age, from the
Corals. ;
Now the ten species, the horizon of which may be of Upper
Khirthar or Lower Nari age, belong to genera whose morphology in-
dicates the presence of totally different physical conditions from those
which environed the stunted, simple, and the few large Corals of the
lower horizon. They were shallow-water and reef-building forms ;
and the genera are Stylina, Latimceandra, Hydnophora, Favia,
Isastrea, Pterastrea, Plesiastrea, and Porites. Thereis nota simple
Coral amongst them ; and the facies is singularly mixed, old and new,
Mesozoic and Cainozoic genera existing together.
The species Hydnophora malirrensis, nobis, is allied to H. venusta,
Catullo, of the European Nummulitic. Porites Pellegrinit, D’Achiardi,
is found in Kurope at San Giovanni Llarione; and Porites indicus, nobis,
is allied to a species from Crosara, Oberburg. The distinctness of
this fauna from that of the Ranikot group is evident enough ; but
it is still Nummulitic in facies and character.
The Narv Series—From the remarks already made upon the
localities of some of the presumed Khirthar Corals, it is as well to
admit that some upheaval took place at the close of that period, and
produced fringing-reef-building or bank conditions. But they did
not prevail throughout the accumulation of the whole of the Nari
Series; and it is somewhat remarkable that no species passes up
from the reef-building horizon into that of the Nari proper.
The genera of the Nari group above the base, indicate rather
vigorous coral-growth, and both deep- and shallow-water conditions.
The genera Trochocyathus, Trochosmilia, Montlivaltia, Cycloseres,
and COyclolites are the simple forms; and the vigorous compound
forms are included in the genera Dasyphyliia, Rhabdophylhia, Lep-
toria, Meandrina, and Prionastrea. | .
The Trochocyatht of the Nari series are remarkable for having
commenced their growth in a discoid shape. Some retained that
shape; but one in particular, Trochocyathus nariensis, nobis, grew
upwards from its disk-shaped base in a perfect cylinder, reaching 2
inches in height.
Trochocyathus cyclolitoides, Kd. & H., is a widely distributed
Huropean Eocene coral, and is found in the Nari series of Sind.
Stylophora pulcherrima, D’Achiardi, from the Hocene of Friuli,
Trochosmilia varicosa, Reuss, from Crosara, Stylocenia taurinensis,
Kd. & H., from European Eocene and Miocene strata, and Cycloseris
CORALLIFEROUS SERIES OF SIND. 201
Perezi, Ed. & H., from the Nummulitic of Nice, are also amongst the
Nari corals. Hence, out of the twenty species of fossil Corals in the
Nari series, one is found at a higher horizon, and one fourth of the
number are found in the Upper Nummulitic and Oligocene deposits
of Hurope.
Taking the Ranikot, Khirthar, and Nari Coral-faunas as a
whole, there are 76 species of Corals in them and severai varieties ;
and of these 16 are identical with European forms which are found
in strata yielding Nummulites to the top of the Oligocene. There
are also eight species in the Sind series, closely allied to those of the
European fauna; and whilst some species are common to the West-
Indian Eocene, an important genus is also common to both localities.
The absence of species passing up from one series to another is
very remarkable.
The Gdj Series——This series of strata contains a large number
of Corals in bands ; but although most of the forms are massive and
compound, and suited for reef-building, the majority are peduncu-
late instead of covering a large surface and incrusting. Some are
very massive ; and the presence of species of Madrepora, an essentially
reef-building genus, with Porites, Agaricia, Echinopora, Prionastrea
Plesiastrea, Brachyphyllia, Leptoria, and Dasyphyllia would
indicate, at the present time, very active shallow-water coral-
growth. The majority of the Gaj genera still flourish; and most
of those which are extinct had the structures requisite for reef-
buildmg. The Astreide as a family preponderate, and simple
Corals are rare, in the collection. But although the facies of the
Gaj coral-fauna is very recent, and there are very few extinct
genera, still the modern Coral-fauna of the Eastern and Red Seas
is not represented by a single species. Two species are identical
with Miocene West-Indian forms; and one is found in the Nari series.
Tt is interesting to find the West-Indian Miocene and recent genus
Antillia represented. Nevertheless the evidence afforded by the
Corals is in favour of a mid-tertiary age being given to the 41
species from Gaj.
In the communication to the ‘ Annals and Magazine of Natural
History’ (1864, vol. xiii.) I described several species of fossil Corals
from unknown geological horizons in Sind; and it is not difficult,
with the lists of the genera and species which have been collected
by the Geological Survey of India, to decide whence the majority
eame. Thus Oculina halensis, nobis, Antillia dentata, nobis, An-
tillia ponderosa, Ed. & H., Cladocora haimei, nobis, Hydnophora
rudis, H. plana, H. hemispherica, nobis, point, with Cyathoseris val-
mondorisiaca, Kd. & H., and Agaricia agaricites, Ed. & H., to a late
Miocene horizon. They were picked up in the neighbourhood of
Karachi, and doubtless came from the highest beds of the Gaj
series.
Finally, many specimens of Isidinee have been found in the Gaj
series; and some of them closely resemble modern forms. No Num-
mulites occur in the Gaj series ; and the Zoantharian eviderce indi-
cates a Miocene age, and not an early one.
202 PROF. P. M. DUNCAN ON THE
The Sindian formations, including the transitional beds with Car-
dita Beawmonti beneath the trap, and the Gaj series at the top,
contain 136 species of Corals and many varieties. Of these, 9
belong to the transitional series, and 56 to strata in which Nummu-
lites exist in profusion. The Nari series, with few species of Num-
mulites and with WV. garansensis, a Kuropean type characteristic of
the Upper Nummulitic or Oligocene, contains 20 species. The
Miocene strata of Ga} contain 41 species. I omit from these
numbers all species from doubtful localities. Thus, as only one
species transgresses, there are five Coral-faunas ; and if the separa-
tion I have proposed at the base of the Nari series is right, there are
six in the same area, included in a prodigious depth of sedimentary
strata. The study of the Corals does not indicate that there was
ever a sea there with a depth of many hundred fathoms; on the
contrary, shallow-water conditions (within 20 fathoms) usually pre-
vailed during the slow oscillation of the area, in which subsidence on
the whole predominated.
IV. The Lquivalence of the Manchhar Strata of Sind and the
Swalik Group of the Himalayas.
The Geological Survey of Sind by Blanford and Fedden has proved
that in some places the Manchhar strata succeed transgressively to
the Gaj series, whilst in others there has been erosion of the marine
deposit before the deposition of the freshwater one, or else the
lower group is absent. Bones of Rhinoceros siwalensis have been
found in the uppermost Gij strata. There is no doubt that the
greater part of the coralliferous strata of the Gaj series accumulated
in shallow water, and yet beyond the reach of the wash-down of a
coast-line. But the lower Manchhars were deposited in shallow
water within the scope of terrestrial denudation. There must have
been considerable general changes in the physical conditions of the
area: and they persisted ; for coral life has never since prevailed
there. The first change probably was one of slight general up-
heaval; and subsequently a slow and progressive subsidence
occurred, during which the vast vertical development (8000 to 10,000
fect at least) of the lower and upper Manchhars accumulated.
Conglomerates, coloured sandstones (grey, green, and red in tint),
and clays, are the prevailing deposits on the inner flanks of the
vast. mountain-system which surrounds Peninsular India, from Sind
to Burma inclusive. Made up of stone brought down by tne rivers
of the extra- peninsular mountain-system, before it became of very
ereat height, and when its breadth was probably much greater than
it is now, these deposits are to be traced to the north of Sind in the .
Suleiman Mountains, in the Salt range, covering much of the
surface of the Northern Punjab, and then, forming part of the sub-
Himalayan range, as far east as the Brahmapootra. Similar
deposits are found, in diminished thickness, in the Assam range ; and
they became important in the Burmese territories. The Sindian suc-
cession of the strata is the normal one; and it extended to a certain
distance northwards ; moreover it is exemplified in the Burmese
CORALLIFEROUS SERIES OF SIND. 203
area. ut in the great central area of the Himalayas proper there
was no marine Miocene. No marine beds, the equivalents of the
Gaj series of Sind and Burma, underlie the Sivalik deposits in the
Sub-Himalayas.
There was open sea during the Nummulitic age where the great
semicircle of extra-peninsular mountains now exists ; and marine con-
ditions persisted on the west and east during the Miocene period ;
but a post-Nummulitic upheaval developed a land-surface and_hill-
tracts from Kashmir to Assam.
This upheaval commenced before, but culminated after, the close
of the Eocene age; and a considerable thickness of purple sand-
stones, red clays, and grey and purple sandstones containing plants
accumulated in the swamps on the plains of that age, near the
mountains on the edge of the Nummulitic sea-floor.
These plant-bearing strata and the underlying Nummulite-
bearing strata have a minimum thickness of 2000 feet, and they
form the Sirmuir series of Indian geologists.
This series underlies unconformably the vast freshwater sedi-
mentary formation comprising the Nahun and Sivalk strata, which
attain a thickness of about 15,000 feet, and, except where buried
beneath recent deposits in one locality, extend, with a varying
development, along the south of the great mountain mass, and are
found on one of the great tablelands to the north of the Central
Himalayan axis. The lower, or Néhun unfossiliferous, series con-
sists mainly of grey lignitiferous sandstones. On it the upper, or
fossiliferous Sivaliks, accumulated as sandstones and clays; and on
the top of all are conglomerates. A great fauna is represented in
all parts of the Sivalik deposits above the Nabun beds.
From the lie of these sedimentary strata, it may be very reason-
ably inferred that the Nahun and Sivalik deposits are the equivalents
of the Lower and Upper Manchhars of Sind; and the inference may
be extended to the Upper Tertiaries of Burma. There is an outlier
of this series and of its lower member in the Gulf of Cambay or
Perim Island.
In attempting to establish exact parallelism between the Sindian
and the Himalayan deposits called Manchhar and Sivalik, it must
be noticed that the vertical development of the last-named rocks is
the greatest, and that whilst the lowest beds of the Sindian series are
fossiliferous, those of the Nahun beds of the Sivdliks are not*. On
the other hand, osseous remains are found throughout the Sivaliks
proper (above the Ndhun beds), but not in the Upper Manchhars
in a recognizable form.
The Manchhar and Sivdlik series have been upheaved, uptilted,
and in the last instance greatly contorted. Both series were the
youngest implicated in the great orographical development; and
although they are on different lines of strike, they were affected
during the same geological period.
The denudation of their exposed edges has been great. Both are
* Possibly the ossiferous deposit at Kushalghar, near Attock, is of Nahun
age. See further on.
204 PROF, P. M. DUNCAN ON THE
covered in some places with high-level gravels; and the Sivaliks of
the great tableland of Hundes underlie deposits referable to the
glacial period, whose effects were not felt so far south as Sind.
In considering the paleontology of these deposit it may be stated
that the osseous remains are found on several horizons.
First, the Rhinoceros-remains which were found included in the
Marine Miocene series of Gaj in Sind, lead to the inference of the
existence of neighbouring contemporaneous land-surfaces and shallow
seas—that is to say, of Miocene land washed by a Miocene sea. The
Rhinoceros, according to Mr. W. T. Blanford, F.R.S., is Rhinoceres
sivalensis.
Secondly, the fragmentary bones and teeth found in the conglome-
rate near the base of the Lower Manchhar formation in Sind accu-
mulated later on than the Gaj series.
The following is the list of the vertebrate remains which were
collected by Mr. Fedden, and named by him and Mr. Lydekker in the
publications of the Geological Survey of India :—
Amphicyon paleindicus. Anthracotherium silistrense.
Dinotherium pentapotamiz. Hyopotomus palzeindicus.
indicum, Hyotherium sindiense.
, Sp. nov. Dorcatherium majus.
Mastodon perimensis. minus.
latidens.
Falconeri. EDENTATA.
Rhinoceros paleindicus. Manis sindiensis.
, sp. near R. deccanensis.
Acerotherium perimense. Rerriita.
Sus hysudricus, Crocodilus, sp.
Hemimeryx, sp. Chelonia, sp.
Sivameryx, 2 sp. Ophidia, sp.
Chalicotherium sivalense.
The conglomerate containing the bones was composed of the
wash-down of the Lower Manchhars themselves.
Thirdly, the fossil bones which have been discovered in consider-
able quantities in a conglomerate on Perim Island (although their
place in the geological series cannot be determined, from the absence
of a succession of rocks) appear to have belonged to a fauna allied
to that of the Manchhars and to that about to be noticed.
The species which have been determined by Falconer and Lydekker
are :—
Dinotherium indicum. Brahmatherium perimense.
Mastodon latidens. Camelopardalis sivalensis.
perimensis. Capra perimensis.
sivalensis. Antilope, sp.
Rhinoceros, sp. Sus hysudricus.
Acerotherium perimense.
The remains are included in sandstone blocks.
The same, or a slightly higher, horizon is recognized far away to
the north, not, however, by its geological position, but by the fossil
remains, in the neighbourhood of Kushdlghar, forty miles south of
Attock, in the Punjab. The deposit contained, according to Falconer
and Lydekker, the following genera and species :—Dznotherwum
CORALLIFEROUS SERIES OF SIND. 205
pentapotamic, Mastodon, Listriodon pentapotanie, Rhinoceros,
Merycopotamus, Dorcatherium, Sanitherium Schlagintweitii, and
Amphicyon palemdicus.
It is remarkable that all these horizons should contain Dzno-
therium.
Fourthly, the Sivalik clays, sands, and conglomerates above the
Ndahun series present an assemblage of genera and species second
to none in importance, and much grander generally than the existing
fauna, which is very slightly represented. A number of genera
which had lived in the Miocene elsewhere were associated with
genera not known in mid-Tertiary deposits, and which have lasted
either into Post-Pliocene or into Recent times. The Dinotheria are
absent. Omitting the common Miocene genera and stating the
others, an African element is noticed, as in the instance of Pikermi
in Greece. The characteristic genera are Paleopithecus, Macacus,
Semnopithecus, Stegodon, Elephas, Lowodon, Hippopotamus, Camelo-
pardalis, Camelus, Bos, Bubalus, Bison, Cervus, Equus, Canis, Ursus,
Mellivora, Meles, Lutra, Enhydriodon, Tapirus, Hystrix, Mus, Rhizo-
mys, Crocodilus, Gavialis, Varanus, Ballia, and Emys.
Moreover many of the freshwater Mollusca are identical with
recent forms.
It appears that these wide horizons are separable into an older
serles, with Dinotherium, Hyotherium, Hemimeryx, Sivameryx, Hyopo-
tamus, Anthracotherium, Acerotherium, and Manis, but without
Elephas and the later bovines; and into a younger series, in which
genera of an African type, such as Hippopotamus and Camelo-
pardalis, are found, and without the older types.
The first series is in relation with the Lower Manchhars, and the
second with the Sivalik deposits above the Nahun beds. But the
interesting fauna from Kushalghar appears to be probably of Nahun
age; and if that should be proved eventually, the succession of two
fairly distinct faunas, linked together by some species, will be
evident.
Finally, the Post-Pliocene deposits of the Jumna area, and also
of the Nerbudda and other peninsular rivers, contain some species of
the Sivalik horizon.
V. General Considerations regarding the Age of the last Himalayan
Upheaval.
It might be supposed, considering the ready manner in which
European mammalian faunas are placed in the scale of geological
succession, that the contemporaneity of some of them with the
Sivalik-Manchhar assemblage of vertebrates would be easily deter-
mined, and a geological age given for the latter without doubt.
But the critical examination of the positions in which many of
the European mammaliferous deposits have been found, indicates
that the manner in which the Tertiary deposits have been classified
by means of the fossil Mammalia is open to exception.
Two well-known examples of European mammaliferous deposits
which resemble, in their succession, the Sivalik-Manchhar series are
206 PROF. P. M. DUNCAN ON THE
those of Eppelsheim and Heppenheim and of Pikermi. At Eppels-
heim sands in small patches are at the top; and they contain a few
specimens of fossil Rodentia, Insectivora, and Carnivora. A con-
glomerate is beneath, and contains the Dinotherian remains, and
also those of Rhinoceros and Mastodon; and all are remanic¢. At
the base of the series there is a clay with freshwater shells; and
it rests conformably on a marine limestone; and this is of late
Miocene age. :
At Pikermi the deposit, the bones from which have been so ably
described by Gaudry and commented on by W. T. Blanford, rests
on a freshwater stratum of Phocene age, and a Miocene lacustrine
series underlies the whole unconformably.
Now at Sind as at Eppelsheim the underlying marine beds are
Upper Miocene in age, and freshwater conditions prevailed subse-
quently, during which the osseous remains were depoisted.
What is the age given to the Dinotherium-conglomerate at Eppeis-
heim? Carl Vogt, influenced apparently by the presence of
Dinotherum, and regardless of any stratigraphical arguments, and
not considering the important changes which had occurred in the
area, in the relative level of the land and sea-floor, decided that the
overlying freshwater beds are of mid-Tertiary age. But Credner,
dealing with the subject more philosophically, and not being so
much impressed with the presence of a genus which elsewhere is
represented in Pliocene strata as by the evidence of the considerable
mutations which had occurred in the physical geography of the
district, and which had brought a marine deposit above the original
sea-level, places the bone-bearing conglomerates in the Pliocene age.
Thus one geologist associates the land and marine elements together,
and the other separates them. |
The comparison which can be instituted between the Manchhar
and Sivalik deposits and those at Pikermi is very close; and, accord-
ing to the ordinary rules of stratigraphy, if the osseous remains at
the last-mentioned locality overlie Pliocene deposits, the animals
which left their bones could not have been of Miocene age. Yet
Prof. W. Boyd Dawkins, in his contributions to this Society, asserts
that the Pikermi fauna flourished in the Miocene. Evidently there
is a great diversity of opinion regarding the age which should be
given to land-surface remains overlying marine strata, freshwater
and estuarine deposits intervening. And if this subject is studied
it will be found that great discrepancies of opinion have existed in
regard to similarly placed deposits in many of the great formations.
About the relative age of some superincumbent terrestrial remains
there is no discrepancy of opinion. ‘The Coal-measures are associated
with the underlying grits and limestones; and the land remains of
the Inferior Oolite are similarly connected in classification with the
marine deposits beneath them. When the lateral extension of the
strata can be traced, and distant marine equivalents of the overlying
series can be proved to contain fossils representative of or identical
with those of the underlying series, the land-surface is classified with
the formation in which the marine strata are placed. Or when there is
CORALLIFEROUS SERIES OF SIND. 207
a succession, on the same area, of marine beds over the terrestrial
and freshwater series, if the fossils of the upper strata resemble
those of the deeply seated marine ones, the whole belongs to one
great aspect of nature.
It will be found that there can be no exception made to placing
the Woolwich and Reading series out of the formation which includes
the white chalk; but the propriety on any grounds of linking the
Purbecks on to the marine Portland is open to exception.
Except im instances similar to those of the Carboniferous and
Inferior Oolite, and where there is also decided unconformity, the
question can only be answered after a careful consideration of the
amount and extent of area implicated in the changes in the physical
geography which may fairly be assumed to have occurred since the
underlying marine deposit was completed. The upheaval of limited
marine deposits recognizable as belonging to a particular formation,
and the accumulation upon them of freshwater deposits and conglo-
merates, would hardly necessitate the belief in such a change in the
aspect of nature as would warrant their classification under two
great geological ages. But when the same phenomenon is witnessed
over widely separated areas, and a conglomerate is followed by some
thousands of feet of fluviatile and other freshwater strata (the
wreckage of high land close at hand), it becomes certain that the
physical change has been wide enough to admit of an alteration in
the geological nomenclature.
With regard to Sind, the Lower Manchhars usually rest conform-
ably on the Gaj marine Miocene, and marine, estuarine, and fresh-
water intercalations exist at their base and before the conglomerate
is fully developed. In one locality the Manchhars rest on a greatly
denuded surface of Gaj strata.
Upheaval (slow, irregular, and on a very grand scale) occurred
subsequently to the deposition of the Gaj series; and ‘a marine tract
became estuarine, fluviatile, and a region of wearing of high land.
Subsequently the enormous subsidence took place, doubtless almost
synchronously with the deposit of the thousands of feet of the
Mafnchhars ; and yet the sea never broke in: it was far away.
The area of change was vast; and it appears to be unreasonable
to associate all these deposits under one geological formation.
The disassociation of the Manchhar and Gaj series is a necessity ;
and the nature of the fauna, so singularly allied to that of Pikermi,
necessitates its relegation to the early Pliocene time.
In following up this subject it must be remembered that the
Sivalik strata, the horizon of which is above the Lower Manchhars,
have a vast vertical as well as horizontal development, and that
osseous remains have been found in them throughout their height.
The fauna as a whole has a later facies than that of the Lower
Manchhars, and resembles, even in its African element, that of
Pikermi. :
On the ground of inferred equivalency with the Upper Manchhars,
and of faunal alliance with the assemblage at Pikermi, it must be
credited that the Sivalik strata are of Pliocene age.
208 PROF. P. M. DUNCAN ON THE
There is another argument which has not hitherto been employed
and which favours this theory.
The Sivdlik strata rest on, or are in contact with (along a line of ©
fault), certain plant-bearing strata of the Sirmur series which are
associated with the underlying Nummulite-bearing Eocene rocks of
Subathu.
The nature of the flora, so far as it has been examined, is not
very foreign to that of India at the present time; and by the same
kind of reasoning which asserts the separation of other terrestrial
and underlying marine strata, these beds, called Kasaoli and Dugr’hai,
may well be the remains of the Miocene land.
Whence were the vast thicknesses of the sands, clays, and con-
glomerates of the Manchhar-Sivaliks derived? ‘They represent a
ruined mountain-chain in bulk; and they are found not only on the
flanks of, but also within, the orographical systems of which they
form parts.
It appears from the study of the history of the Himalayas by
Strachey, Stoliczka, Medlicott, and those Indian Geological Sur-
veyors who have laboured so industriously of late years, that a low
mountain-chain existed on the area after the Nummulitic age—the
results of a post-Nummulitic earth-movement. It was probably
a broad chain, and not a sufficient barrier to prevent the roaming of
the animals on and over it in the subsequent geological age. This
chain appears to have had an axis of old rocks; and the whole
suffered denudation during the age of the Sivalik Mammalia. In
Hundes Strachey found the great tableland (now at an altitude of
from 14,000 to 16,000 feet) to consist of sediments filling up a basin
in old rocks to the depth of 3000 feet—sediments which included
osseous remains of animals that could not have traversed high and
difficult mountain-ground. .
Part of the Sivalik sediments were formed out of low mountain-
ground by fluviatile denudation; but to account for the vast deve-
lopment of the rest on the flanks of the present mountain-system, it
is necessary to admit that the upheaval, and much of the north-and-
south crush of the Himalayas, occurred part passu with the slow
accumulation. Elevation and diminution of the breadth of the area
progressed ; and doubtless much of the great crush which folded and
often reversed the flanking strata was final.
The Sivalik strata rest on the flanks of the chain and on old rocks
within the range; and they were the youngest deposits affected by
the mountain-making. Hence the Himalayas, as a grand system,
culminated during and subsequently to the collection of these strata,
which have been pronounced to be Pliocene in age.
The Sivalik deposits in the tableland of Hundes are overlain by
relics of the great glacialization of the Himalayas. Hence, before
the vast glaciers of the glacial period accumulated, valleys had been
Worn out and denudation had proceeded. So it is necessary to
recognize that the culmination of the movements which developed
the height of the Himalayas occurred in preglacial times and
during the Pliocene age.
CORALLIFEROUS SERIES OF SIND. 209:
To complete the serial changes, it is to be remembered that a
Postglacial fauna was found in the old alluvium of the Jumna,
a wash-down of the Himalayas.
With regard to the Upper Manchhars, they were implicated in the
great orographical movement, which was contemporaneous through-
out the extrapeninsnlar area of India; and they are of Pliocene age.
The details regarding the succession of strata and of many of
their organic remains are to be found in the publications of the
Geological Survey of India, and in the communications to this
Society by Strachey, Grant, Falconer, and others. The ‘Manual of
Indian Geology, by Medlicott and Blanford, an abstract of the
labours of the Survey, contains them in a condensed form. I am
under great obligations to all those writers, and also to Messrs. Med-
licott and Blanford for much unpublished information ; and in thus
heartily acknowledging my obligations, I am glad to have the
opportunity of expressing my assent to their conclusions regarding
the age of the Himalayas.
Discussion.
The Presrprent remarked on the persistence of Mesozoic types in
the Tertiary strata of the Himalayas.
Mr. Branrorp expressed the obligations of himself and other
Indian geologists to Dr. Duncan for his researches on the Corals.
which they had collected. The base of the series of Sind consists
of a limestone containing Hippurites; and above these Cretaceous
beds are strata partly unfossiliferous and the representatives of the
Deccan traps, the whole being overlain by the Lower Eocene and
Nummulitic. This succession is shown both in the Laki and the
Khirthar ranges. The Nari or Oligocene group is 5000 or 6000
feet thick ; its upper subdivision, which is much thicker than the
lower, is of freshwater origin, and contains imperfect plant-remains.
This is overlain by the Gaj and Manchhar. The unconformities which
occur in the series are purely local. He was gratified to find
that Dr. Duncan had arrived at the same conclusion as the Geolo-
gical Survey of India as to the age of the Sivdlik beds. He
replied to the opinions expressed by Prof. Boyd-Dawkins and
Mr. Bose on this subject.
Lieut.-Col. Gopwiy-Auvsten remarked upon the greater contortion
of the Nummulitic strata in the Western Himalayas as compared
with those of Assam.
The Autor stated, in reply to the President’s remarks, that
while the genera of Corals are remarkably persistent, the species are
not. He bore testimony to the great value of the volume published
by the Geological Survey of India. He doubted the value of the
terrestrial Mammalia as fixing the age of the strata overlying the
Kocenes.
210 C. CALLAWAY ON THE ARCH XAN
15. The Arncoman Guotocy of Anetusny. By C. Carraway, Hsq.,
M.A:, D.Sc., F.G.S. With an Appenprx on the Microscopic
SrRuctuRE of some ANGLESEY Rocks, by Prof. T. G Bonney,
M.A., F.RB.S., Sec.G.8. (Read January 5, 1881.)
[Prats VIIT.]
Introduction (p. 211).
A. Description of Areas and Sections.
i. Menai Anticline (p. 211).
a, Gmeissic series.
(1) South of Pentraeth.
(2) Mynydd Llwydiarth.
(3) Gaerwen to Menai Bridge.
b, Slaty series.
If. Llangefni “Syncline” (p. 215).
a. Slaty series.
(1) Llangristiolus slates and grits.
(2) Llangefni conglomerates and shales.
(3) Cerrig-Ceinwen slaty and calcareous group.
6. Gneissic series.
(1) Coast section from Porth Nobla to Aberffraw Sands.
(2) Railway-section from Ty Croes to Bodorgan.
(3) Distribution of the subdivisions in localities to the north-east.
IIY. Central Zone (p. 218).
a. Slaty series.
6, Gneissic series.
(1) Bodafon Mountain.
(2) Section between Llangwyllog and Llanerchymedda.
(3) Area south-east of Paris Mountain.
(4) Structure of the Zone.
ITV. Northern Area (p. 221).
(1) Voleanic group of Paris Mountain.
(2) Chloritic schists of Mynydd Mechell.
(3) Llanfechell grits.
(4) Rhosbeirio shales.
(5) Sharply contorted group south-east of Amlwch.
(6) Slates and limestones of Amlwch and Cemmaes.
Y. North-western Area (p. 224).
Section from Porth y defaid to Pen bryn ’r Eglwys.
VI. Western Area (p. 225).
(1) The Mainland. .
(2) Holyhead district.
(3) Rhoscolyn district.
B. Summary of Results.
1. Distribution of the Rocks (p. 227).
a, Gmeissic series.
(1) Geographical.
(2) Stratigraphical.
b. Slaty series.
Ii. Evidence of Age (p. 229).
a. Relations to Palzozoic groups.
6. Relations to each other.
c. Relations to other areas.
(1) Caernarvonshire. (3) Shropshire.
(2) St. David's, (4) Charnwood.
Conclusions (p. 232).
Appendix (p. 232).
eee ee ee
Quart. Journ. Geol, Soc. Vol. XEXVIL. Pl. Vill
Fig. 6. Section ir lower Quarry, Nebo.
Fig. 5. Section in upper Quarry, Nebo,
jes =
yy en ob s
U Yf S S
Uf)
Yi
Yi
Fig.3. Section across lynydd Llyydiarth .
we a a OT Oy
Mi
,
'
.
‘ ‘
‘
as v
, he 4
i
Quart. Journ. Geol. Soe. Vol. AMV Pl. Vi
Fig. 6. Section in lowe Quarry, Nebo.
Fy. 1.
MAP of ANCLESEY
Fig.2.; Generalized Section trom Holyhead Mountain to Menar Strats.
ESE. 5.5.W. EE. Malllraeth
Tlangefne Marsh
Werrrre EMAL A=
Ss
with a, overlying
Fred* Donyerlield Lith Lorudon
18
GEOLOGY OF ANGLESEY. PU:
INTRODUCTION.
[I wave to submit evidence in support of the conclusion that there
are represented in Anglesey two Precambrian or Archean groups,
each distinguished by well-marked lithological characters. They
may be named respectively the Slaty and Gneissic formations. The
‘“‘ Pebidian ” schists, as recognized by Dr. Hicks, I include in the
eneiss group ; but, in other parts of the island, I have worked out
a great assemblage of fragmental felspathic rocks, which I believe
to be of true Pebidian age. I shall also attempt to prove that the
quartz rocks of Anglesey are included in the gneissic series. ‘The
microscopic notes, kindly furnished by Prof. Bonney, are based upon
the specimens only, and have all the value of independent evidence.
The growing importance of these ancient rocks would seem to re-
quire that the provisional term ‘“ Precambrian” should give place
to a word which can be permanently used; and I have ventured to
adopt the term “‘ Archean,” so widely employed by Continental and
American geologists. To the words ‘“‘ Azoic” and “ Hozoic” there
are obvious objections.
A. Description oF AREAS AND SECTIONS.
I. Menat ANTICLINE.
For convenience I accept this name for the rocks lying between
Menai Straits and the great fault which throws down the newer
Paleozoic rocks of Malldracth Marsh, though the term is not strictly
applicable. It is true that the strata on the south-east side of the
area dip to the south-east, and those on the north-west side to the
north-west; but between these two extremities the undulations are
frequent, and some of the dips are probably overthrows.
a. Gineissec Series.
_ wo Varieties of Gnerss—The structure of the area is rendered
much clearer by the recognition of two prevailing gneissic types—
a dark micaceous or hornblendic variety, associated with chloritic
schists*, and a greyish or light-red rock clearly foliated into an or-
dinary ternary gneiss. in the Craig-yr-allor anticline ft the two
varieties are also recognizable, the grey gneiss passing up through
the dark type into the granitoidite. In the Menai district the dark
schist holds the same relation to the grey variety, and the passage
between the two may be seen at many points.
1. Gneiss south of Pentracth.—Next to the fine section at Gaer-
wen #, the rocks south and east of Pentraeth require notice. The
band coloured “ greenstone,” running from Tai hirion north-north-
east to Plas-gwyn lodge, appears to be a highly-altered hornblendic
gneiss, with a north-west dip. In the field to the south-east of the
lodge is a small quarry of typical grey gneiss; and in the plantation.
* Throughout the paper the terms “schist ” and “schistose ” are strictly con-
fined to foliated rock.
t Geol, Mag., March 1880, p. 119. + Geol. Mag., March 1880, p. 121.
Dal C. CALLAWAY ON THE ARCH HAN
a few yards to the north-west we find the dark-green schist in its
usual position above, both dipping to the north-west.
Following the strike to the north-east, the gneiss is seen to con-
tain angular pieces of quartz, some of which are flattened in the
foliation-planes, so as to appear like ordinary folia.
2. Mynydd Llwydiarth.—This elevated ridge, trending to the
north-east for nearly a mile and a half, is composed of highly con-
torted gneiss. The general dip is north-west; but in some places
the beds undulate to the south-east ; and the thickness cannot be
great. The rock is more quartzose than usual; and the quartz frag-
ments become much more numerous,—the two facts suggesting the
proximity of quartz land. The gneiss, rolling in frequent contor-
tions, is finely exposed in low vertical cliffs ; and the angular pieces
of white quartz studding and projecting from the surface produce a
very striking effect. Both types of gneiss appear to be present;.
but the felspar being less abundant, the rock is brought into closer
resemblance to the micaceous and chloritic schists of Holyhead. On
the north-western slope the gneiss is extensively brecciated, and
the presence of a fault is further inferred from an abrupt transition
to younger formations. At the foot of the slope, near the fault, the
eneiss becomes somewhat granitoid, suggesting the commencement
of the passage into granitoidite, which is seen so clearly in the Craig-
yr-allor anticline. At the extreme north-east of the ridge, on Red
Wharf Bay, the green schist is exposed for some distance across the
strike to the east ; but south of Wern we come onto the grey gneiss,
all the dips being north-west. Further to the east, at Bryn y Castell,
the grey type is again seen, but with the dip reversed; and at Hafodty,
still further to the south-east, the dark schist comesin again. This
is a clear anticline, the grey gneiss exposed at the apex throwing off
green schist in opposite directions. The structure of this district is
shown in Pl. VIII. fig. 3.
3. Gaerwen to Menart Bridge.—Crossing the anticline from Gaer-
wen, we find at the railway-junction that the dark schist has rolled
over to the south-east; but half a mile to the south-east, near
Llanddaniel, the series, represented by contorted quartzose chloritic
schist, dips north-west. Exposures then are rare till we come to
the Anglesey column, where dips are in opposite directions, but
usually to the north-west. This rock is of the ordinary dark green
type, occurring everywhere above the grey gneiss in both the Menai
and Craig-yr-allor areas. It has been described by Prof. Bonney *.
On the Straits, near the west end of Menai Bridge, green schists
occur of the ordinary varieties.
From the above facts it is clear that the rocks of the anticline
belong to the gneiss series. Well-foliated gneiss occurs at numerous
localities; and the green schist 1s so intimately associated with it,
as an upper band, as to remove all shadow of doubt that the two
types form one unbroken group. In this area I have not found a
trace of any thing but true crystalline schists.
The thickness of the group is not great. The foldings are nume-
* Quart. Journ. Geol. Soe. vol. xxxv. p. 308.
GEOLOGY OF ANGLESEY. 213
rous, the lower gneiss being brought up to the surface at many
points. Probably the entire series is exposed west of Gaerwen,
where the total thickness can hardly reach 1000 feet.
An isolated mass of schist occurs south-west of Pentraeth. It is
about a mile long by half a mile broad, and is bounded by faults on
all sides. Carboniferous Limestone surrounds it on three sides. On
the east it is separated from the main mass by a faulted strip of the
formation now to be described.
b. Slaty Serves,
This wedge is composed of rocks of a newer Archean group.
At Tan y graig, south-west of Pentraeth, is a greenish, coarse,
slaty variety. In the fields to the north-west, a jaspery rock
projects in small knolls through the turf; but its relation to
the bedded type is obscure. Crossing a hollow to the east, we
come to a ridge, the western slope of which is occupied by
massive breccias. The fragments and the matrix are similar, and are
composed of a grey and purplish dolomite (Note 40, p. 235). Further
to the north-east, above Wugan bach, is a light-purple slaty rock,
which in places is literally smashed. Between this point and Plas
ewyn, along the ridge, the prevailing type is a purplish ashy rock,
sometimes brecciated, and in places altered almost to a hornstone.
The dip is high to the north-west. The breccias of this ridge are
obviously connected with faulting. North of Plas gwyn, on the
same strike, is a puzzling rock, which, under the microscope (Note
41, p. 236) appears to be a limestone rendered impure by volcanic
mud. Slaty beds are again seen to the north-east of Pentraeth,
dipping south-east.
For the greater part of its length this mass is separated from the
Menai anticline by a faulted strip of Paleozoic shale; but north-
east of Rhiwlas it comes up against the gneiss, the fault between
the two formations running along a hollow. The heavy breccias
which fringe both groups point to excessive fracture and crushing.
Il. Luaneernt *‘ SyNcLINE.”
Crossing the Carboniferous strata of Malldraeth Marsh, we come
to an altered and contorted group of rocks which bear a superficial
resemblance, especially in their colour, to the Menai schists, and
have hitherto been regarded as a part of the same group. But on
a careful examination of the lithology of this series, fundamental
differences are observable. Even my first day’s work in the district
convinced me of the existence of Pebidian rocks of the St.-David’s
type; and fuller working-out of the area brought to light analogies
with other Pebidian localities.
Slaty rocks occupy only the south-eastern side of the apparent
syncline lying between the Carboniferous on the south-east and
the granitoid band on the north-west, the north-western side being
composed of gneissic strata. The two groups are brought together
by a fault or faults; but as they dip towards each other, an appa-
rent basin is formed (see section near Aberffraw, Pl. VIII. fig. 2).
Q.J.G.8. No. 146. f°)
aa C. CALLAWAY ON THE ARCHAZAN
a. Slaty Serves.
1. Llangristiolus Grits and Slates—The lowest beds I have ob-
served are exposed near the Llangristiolus turnpike. The rock is
clearly bedded; but its lithology is obscure, and the jointing is so
close that clean fractures are hard to get. It appears to be a quartzo-
felspathic grit, altered into a sort of hilleflinta. Some bands are
coarser, grains of quartz and ielspar being visible to the naked eye.
A similar rock is common in the Pre-Cambrian rocks of the Chureh-
Stretton district (Shropshire).
A little further to the north, near Cerrig ddwyffordd, a quarry-
section is very interesting. At the base is a purplish grey felspathic
grit (Note 42, p. 235). This is overlain by a pale-green slaty rock of
Charnwood type, associated with, and apparently passing into, a
sort of porcellanite (Note 43, p. 234), singularly like a rock at Caer
bwdy, St. David’s. ‘The Charnwood facies of these varieties is also
noted by Prof. Bonney. The section is capped by a repetition of
gritty bands. The dip is northerly, at from 40° to 50°. Similar
rocks are exposed in neighbouring fields.
2. Llangefni Conglomerates and Shales.—TYo the west and north-
west of the Llangristiolus sections are several exposures of a greenish
conglomerate. ee is seen on the Holyhead road, near Waen She and
north of Cerrig ddwyffordd, at the arrow mark, but is ver y fully ex-
posed in the railway- -cuttings north-west of Llangefni, the enclosed
fragments, weathering white, being clearly visible even from the rail-
way carriage. The matrix is green shale. The pebbles are very
varied, the following being the principal types :—quartzite, common ; |
pinkish grit (Note 38, p. 235) of quartz and felspar; greenish fel-
spathic grit; and green and grey hornstone. Of these, quartzite is
the only ingredient which is certainly foreign to the slaty series ; the
others are such as are found in some part of the group. The con-
glomerate would then seem to have originated in contemporaneous
denudation, such as is common in yolcanic rocks, together with the
wearing-down of a preexisting land composed of quartzite.
Interstratified with the conglomerate are beds of purple and
green felspathic shale, with some bands of hornstone.. The resem-
blance of these rocks to the St.-David’s types is unmistakable.
The road-sections in this district display a prevailing north-west.
dip; but the more complete exposures in the railway-cuttings
reveal frequent undulations, so that the thickness is not great.
A similar group, probably on the same horizon, is well displayed
in the cuttings east of Bodorgan station, 6 miles south-west of
Llangefni. The prevailing rocks are purple, green, and grey ashy
shales, with some felspathic breccias. Conglomerates occur con-
taining pebbles of felsite, in which microscopic examination (Note 39,
p. 236) reveals a very interesting resemblance to modern lavas.
Associated with the shales at Llangefni station is a thick bed of
quartzose grit, such as might have been preduced by the denudation
of an ancient quartzite.
Still following the strike to the south-west, we find the slaty
series well exposed at numerous points on the coast from Bodowen
GEOLOGY OF ANGLESEY. 215
round to the Aberfiraw sands. On the shore near Bodowen, Llan-
gefni conelomerate is underlain by grit. On the east side of Porth
twyn mawr, it overlies slaty rock, and contains large unrounded
pieces of it. The same conglomerate, repeated by folding, occurs at
intervals as far as the Aberffraw sands.
Quartzite occurs in lenticular bands in pale-green slate west of
Porth Cadwaladr. This association is also very common in Northern
Anglesey. :
Near, or at, the base of the slaty series of this district are several
masses of quartz rock of obscure origin. The most prominent of
these is the craggy hill* called Craig fawr, above Llangefni. It
1s a massive white rock, in which the quartzite structure is still
apparent. It is surr ounded by Carboniferous strata, and it probably
formed an island in the Carboniferous sea. The same rock may be
traced at intervals along the strike to the south-west. One conspicuous
crag of it is seen at Bethel, north-east of Bodorgan station. I can
only suggest that we may have in these bosses the remains of an
ancient land, from which the Pentraeth gneiss derived its angular
fragments, and the Llangefni conglomerate its rounded pebbles and
its quartz grits.
3. Cerrig-Ceinwen Slaty Group.—These rocks lie to the north-
west of the last group, with the same (north-west) dip ; and as they
present important lithological differences, they can hardly be repe-
titions.
North east of Cerrig Ceinwen, a little south of the Holyhead
road, are green and purplish slaty beds. Some bands are calcareous ;
and the formation on the whole resembles the rocks forming the
ridge at Wugan bach. Large nodules of jasper are abundant. Their
origin is not absolutely clear; but 1 am disposed to regard them as
included pebbles. The beds have a high dip to the north-west.
On about the same strike to the south-west are pale green ashy bands.
Close to Cerrig-Ceinwen church, to the north, are prominent ridges,
composed of a greenish rock, so tough that it was difficult to obtain a
specimen. It has a superficial resemblance to a greenstone, but is
undoubtedly an indurated sedimentary rock, presumably an ash. It
suggested the “‘ greenstone” of Clegyr Foia, St. David’s.
A fine exposure in a quarry west-south-west of Cerrig Ceinwen,
on perhaps a little lower horizon than the jasper conglomerate,
deserves attention. The rock is typical of the slaty series of
Anglesey. In the field it appears asa pale green slate or indurated
shale, sometimes faintly banded. Comparing it with some of the
Charnwood slates (Note 44, p. 234), the only difference I could detect
was that the Anglesey type displayed a slight lustre indicative of
incipient metamorphism. It sometimes passes into a rock in which
the alteration has been carried further, sometimes into a sort of
hornstone. ‘The dip is still to the north-west.
At Bod enlli we are apparently on the horizon of the jasper
conglomerate. The conglomerate itself is not exposed; but we have
limestone, purple slates, and green breccias and shales, not unlike
those associated with the j jasper.
* Coloured ‘‘ greenstone” on the map.
216 C. CALLAWAY ON THE ARCH AN
Over a mile to the west-south-west, at Cerrig engan fawr, there
is a considerable exposure of a very tough, green, ashy-looking rock,
similar to the variety north of the church.
All the above rocks dip to north-west ; but a little further to the
west, at Ty’n-y-buarth, the beds dip to south-east. The strata at
this locality are highly contorted on a small scale, and are very
similar to the gnarled rocks east and south-east of Amlwch, the
alteration, as in that district, having proceeded further than at
Cerrig Cemwen. In all other respects these altered rocks resemble
the Cerrig-Ceinwen slates. '
b. Gnerssice Serves.
The band of gneissic rocks is hardly a mile in width at Bodwrog,
where it is separated from the Pebidian by a faulted strip of Pale-
ozoic shale ; but it gradually expands to a breadth of over two miles
in the coast section on the south-west. The fault separating it
from the slaty series runs from near Bodwina, north of the
Holyhead road, in a south-south-west direction, losing itself under
the sands of Aberffraw. On the west of the sands are nothing but
schists ; on the east are nothing but rocks of the slaty series. It
will be necessary to describe two sections across this zone.
1. Coast Section from Porth Nobla to Aberffraw Sands.—On the
coast, west of Porth Nobla, is a considerable exposure of greenish
felspathic rock similar to the halleflinta seen on the strike to the
north-east, near Ty Croes. It appears to form an anticline. On
Porth Nobla it clearly dips south-east, and passes gradually up into
grey gneiss. To the west it presents but slight indications of
Stratification ; but as we proceed eastward planes of separation grad-
ually appear, which, at first obscure, become more and more distinct,
till the rock is undistinguishable from a true gneiss. I have long
since noticed an unbroken passage between hilleflinta and gneiss
in the Wrekin; and Dr. Hicks has recorded the presence of an
incipient foliation in the hilleflinta (‘‘ Arvonian’’) of St. David’s.
The grey gneiss soon passes up into quartzose gneiss, quartz-schist,
and quartzite. These siliceous types, which are of much theoretical
interest, occur in great force, and form the main part of the
headlands of Mynydd baen and Pen y cnwe, which project between
Porth Nobla and Porth Trecastell. On the west side of Porth
Trecastell is a band of calcareous quartz-schist, or quartzose foliated
limestone. The silicate appears to be tale or chlorite. ‘There is
a break in the section at the centre of the bay; but as the cal-
careous schist reappears on the east side, there can be but a slight
break, if any, in the succession. Overlying the last-named rock is
a considerable exposure of decomposed grey gneiss interstratified with
bands of quartz rock, the whole being much contorted and broken.
A greenstone dyke appears here. After a few undulations, the de-
composed rock disappears, and ordinary white and grey gneiss, some-
times rather quartzose, dips steadily to the south-east for some
distance. Then comes in the well-known green schist of the
Menai type, which is continued to the Aberfiraw sands. It is well
GEOLOGY OF ANGLESEY. ATE
seen on Porth gwyfen with the normal south-east dip. On the
shore, near the church, an undulation brings up grey gneiss.
Then the south-east dip is resumed; but at Trwyn du, just before
reaching the Aberffraw estuary, the beds turn up to the south-east,
and a syncline is formed. The sucgession described is shown in
fig. 4.
52. Section on the Railway from Ty Croes to Bodorgan.—tThe suc-
cession is substantially the same as the last; but it furnishes one
or two additional facts. At Felin bont is the hilleflinta first
noticed by Dr. Hicks, who rightly conjectured, as the last section
proves, that it passed to the south-east beneath the schist at Ty
Croes*, though he was in error in placing it above the granitoidite,
which les at the very summit of the gneiss series. West of Ty
Croes quartzose schist is exposed in the road.
Coming to the railway-cuttings, we find to the east of the station a
good section of grey quartzose gneiss (Note 34, p. 233) dipping south-
east. This rock is one of the most prominent types seen west of Porth
Trecastell. Grey and white gneiss are seen for more than a mile
with the same dip. In the cutting from near Bodgedwydd to near
Graig bach, the grey gneiss grows gradually darker and darker, and
passes without a break into the dark green Menai type, which is
continued to the end of the exposure. The average dip is 40° to
south-south-east. Leaving the line, we find in a road-section north-
east of Tre’ Iddon that the dip of the dark schist has changed to the
north-west. Hast of this point we come almost at once to the slaty
beds and conglomerates of the newer series.
The railway-section is thus seen to agree precisely with the suc-
cession on the coast. In some points it is less complete; but it dis-
plays very clearly the passage of the grey into the dark schist, so
well seen in the Menai anticline.
3. Distribution of the gneissic Subdivisions to the North-east. Halle-
jinia.—This band gradually narrows towards the north-east, being
cut out by the fault that brings the lower part of the gneiss series
against the granitoidite ; so that at Gwalchmai it is hardly visible,
and at the section; north of the Holyhead road the grey gneiss is
in immediate contact with the granitoidite. Some of the gneissic
rocks of Gwalchmai display a transition towards the halleflinta
types.
Quartz-schist. This zone is not well exposed near ‘'y Croes. To
the north-east it is seen at Melin Ddrydwy andGlan’rafon ; but it may
be best studied at Gwalchmai near the church, on the road to the south-
west of the church, and on the Holyhead road. In the last locality
the granitoidite is brought against it by the fault. The dip is to
the south-east, except on the Holyhead road, where it is reversed.
There is probably a broken anticline at this point. The prevailing
* I was at first disposed (Geol. Mag. March 1880, p. 128) to associate this
halleflinta with the granitoidite, since similar rock, together with quartz-
felsites, is included in that group; but the coast-section has cleared up several
difficulties.
t Geol. Mag. March 1880, p. 124.
21
oa)
C. CALLAWAY ON THE ARCHAAN
type is a true quartz-schist, sometimes passing into a quartzose
eneiss. As it was important to critically compare this rock with
the quartz rocks of Holyhead and Bodaton Mountains, I have had
four specimens cut; and Prof. Bonney appends full descriptions
(Notes 25-28, p. 233).
Grey Gneiss. From the section east of Ty Croes station, this
band may be traced to the north-east, forming the low ridge from
Tal y llyn to Gwalchmai. Passing to the east of Gwalchmai church,
it 1s well exposed about Bodkin tae. and on both sides ef the
marsh (Cors Bodwrog) and pool. At Bodwrog church it is in contact
with granitoidite, the quartz-schist having in its turn been cut out.
In the ridge to the east of the church the gneiss is interstratified
with a highly crystalline limestone, or calcite-schist (Note 51, p.236).
From the microscopic description 14 will be seen that this rock re-
sembles the quartzose limestone of Porth Trecastell ; and it is pro-
bably on the same horizon. The normal south-east dip is preserved
as far as the old Holyhead road, north of the marsh ; but near here
a change takes place, and black Paleozoic shales come up to the
eranitoidite.
Dark Schist. This zone is not well seen north of the Holyhead
railway. The fault which limits it on the south-east gradually cuts
it out, so that east of Gwaichmai the slaty series approaches the
grey gneiss. The gneiss is exposed at Pen bryncele, dipping south-
east ; and half a mile to the south-east, near the +2 milestone on
the Holyhead road, we find green slaty rocks with a north-east dip.
IIL. Centrrat Zone.
This band extends across the island from sea to sea. It is the
most complicated part of this broken and contorted area; but by
steady attention to the lithology, assisted by some stratigraphieal
indications, clear results may be secured.
a. S laty Series.
In following up the gneissic rocks towards Bodafon Mountain in
order to ascertain the relation between the gneissic and quartz
groups, I was surprised to find an area of slaty rocks between the
two. At Plas Llanfihangel dark gneiss and granitoidite dip to the
south-west; and a little further to the north, at Ma’n-addwyn,
felspathic shales dip as if they would pass below the gneiss. The
rock is of a typical St.-David’s type, and unquestionably pelongs to
the younger series. High up on the south-east slope of the moun-
tain are similar rocks dipping south-east. The dips in both cases
being away from the quartz rock, it was natural to infer that the
shales rested immediately upon it. Further examination proved
that such was not the case.
At the south-west end of the quartz ridge north-west of Tyn—
‘Wlidiart the flanking rock is a sort of hornstone, banded pink and
green, of a common Pebidian type. Approaching the hill, the horn-
stone is seen to dip away from it to the south-west; but surmounting
the low ridge made by the. hornstone, the beds are observed to roll
GEOLOGY OF ANGLESEY. 219
over and plunge directly towards the quartz at the very junction.
A little further to the north, above the farm, the evidence of dis-
cordance is, if possible, still clearer. In the quarry is a good section
of a greenish slaty rock, with the beds striking directly at the quartz
forming the ridge at a distance of about 20 yards.
It is thus evident that the slaty series is faulted against the quartz
group of Bodafon Mountain.
b. Gneassic Series.
1. Bodafon Mountain.—This mass cannot be brought into direct
stratigraphical relation with the gneiss group, for the reasons just
explained; but the lithological resemblance of this rock to the
quartz-schist of Gwalchmai and Mynydd baen is so close as to
render the correlation highly probable. In hand specimens some of
the varieties are undistinguishable. Prof. Bonney, who was not
aware of my views when working on the specimens, groups a typical
variety (Note 29, p. 233) from the summit of the mountain with
the Gwalchmai schists. The rock of the western ridge, which is a
little more schistose, is also closely represented in the south-western
localities. The inlier, surrounded by newer Paleozoic rocks, which
lies to the south-east is precisely similar to the eastern part of the
hill.
2. Section between Llangwyllog and Llanerchymedd.—The sue-
cession between these points is similar to that of the coast-section
between Ty Croes and Aberfiraw; but the granitoidite is wanting
in the latter, and the dip is reversed, so that the two sections repre-
sent the two sides of a broken anticline.
The granitoidite occupies a large area south of Llanerchymedd.
Round Coedana is a grey variety, rather small-grained. To the south,
at Rhydgoch, it is much coarser, consisting of fragments of pink
felspar in a matrix of smaller bits of quartz, felspar, and chlorite.
The older geologists would have called it a porphyritic granite.
The dark: schist is exposed about half a mile further to the south,
at Glanrhyd, being the band of “ greenstone” of the Survey. Prof.
Ramsay originally suspected the metamorphic origin of this rock ;
and, after microscopic examination,: Prof. Bonney is disposed to
consider it a hornblendic gneiss, containing felspar, epidote, horn-
blende, and some quartz, the felspar being decomposed, and the
whole a good deal “‘ messed.” Any obscurity arising from such an
altered rock is removed if we follow the strike to the north-east.
To the south-west of Graig Ilwyd there is a good exposure of
hornblendic gneiss interstratified with granitoidite. The gneiss
sometimes passes into hornblende-schist. The hornblende is well
erystallized ; and the alteration is very slight.
The grey gneiss is well seen about two furlongs south of Glanrhyd,
in a quarry north of the stream. The dip is high, to the north-west ;
and the rock is of the ordinary type.
No rock is seen on the road for two or three furlongs to the
south ; but north of Llangwyllog church there is a slight exposure
of hallefinia too small to display dip. There is room for the
220 C. CALLAWAY ON THE ARCH EZAN
quariz-schist between this rock and the grey gneiss; but I cannot
affirm its presence.
3. Arca south-east of Paris Mountain.—Vhe gneissic rocks of this
district are on the north-easterly prolongation of the strike of the
central zone; and there is no doubt that they belong to the same
series: the dip, the succession, and the prevailing rock-types are
the same.
On the coast between Dulas Bay and the fault north of Porth
lygan the succession is not satisfactory, owing to great disturbance.
South of Porth lygan the shore is mainly occupied by sandstones
and conglomerates, presumably of newer Paleozoic age, deposited
on an eroded surface of gneiss, and sometimes wrapping round little
promontories of the older rock. ‘The prevailing dip is easterly. On
Porth lygan the gneissic series is well exposed. Grey gneiss, dark-
green schist, granitoidite, and quartzite (all the types which occur
on the strike inland) lie in confused, contorted and shattered masses.
At the north of the bay the rocks are less disturbed, and dip to the
north-west. Black Ordovician (Lower Silurian) shales are faulted
down to the north, resting, in a clear coast-section, against the
granitoidite.
Between Llanwenllwyfo and Nebo the succession is more dis-
tinct. Thin-bedded gneiss is seen at several points north-west of
Llanwenllwyfo and north of Plas uchaf; the overlying green schist
is well exposed around Rhos manarch; and the capping grani-
toidite, with associated schist-bands, forms the ridge between Nebo
and ‘'y-Newydd, the whole dipping to the north-west. In two
quarrics south-east of Nebo there is well exposed a strong band of
quartzite and quartzose conglomerate, similar to some of the masses
on the coast. I have elsewhere* given reasons for believing that
this is the equivalent of the quartzose conglomerate of Twt Hill;
and I stated that in these quarries the rock is unconformably oyver-
lain by black shales of (at least) Bala age. If the shales are
Tremadoc or Arenig, as Prof. Hughes has since maintained, the fact
is still more strongly confirmatory of the Archsan age of the
quartzite. As the point is important, I submit a section (figs. 5 &
6) from each of these quarries.
Since this quartz-rock is Precambrian, is conformably underlain
and overlain by gneissic strata, and occurs on the coast in the closest
association with gneiss and granitoidite, there can be no hesitation
in referring it to the older Archean series. It must not. however,
be confounded with the quartz-schist of Bodafon Mountain, which is
lower in the succession.
Granitoidite and dark schist are found along the ridge to the
west, and at the base of Paris Mountain. I have not examined the
latter locality ; but Mr. Allport kindly allows me to use some notes
made by him in May 1868. The numbers refer to specimens now
in the British Museum.
“443, Fine-grained granite? South-east flank of Paris Mountain.
“444, Granite? 100 yards from last.
* Geol. Mag. March 1880, p. 118.
GEOLOGY OF ANGLESEY. DN
© 338. Hornblende-schist, passing into a more compact rock (339),
not schistose, or very slightly so; and this, again, into hornblende
and felspar rock, very similar in appearance to that at Malvern (340).
‘«‘This is an interesting case, as the above varieties were taken
from different parts of the same large block. As in Malvern rocks,
epidote occurs near the joints. No.340 might be called hornblendic
eneiss; the felspar 1s well crystallized in many parts of the mass.
In this place there is also hornblende and mica rock; and in some
parts hornblende and felspar occur in separate layers. The granite
has a gneissose structure; and to my mind the evidence is clear that
the whole form a series of metamorphic rocks.”
I am glad to quote confirmatory evidence by so competent a
ithologist, and trust that it will be unnecessary to multiply retuta-
tions of the old “‘ granite-vein”’ hypothesis.
A, Structure of the Zone.—-For structural purposes it is necessary
to include in this band the gneissic area between Ty Croes and
Aberfiraw. The whole forms a complex and shattered anticline. A
central fault margins the granitoidite on the east from Caernarvon
Bay to a mile north-east of Bodwrog; then 16 curves a little to the
east, and, passing near Llangwyllog, leaves room for the underlying
gneisses. ‘The strata dip in opposite directions on each side of the
fault. This dislocation thus appears to pass along the summit of
the anticline; but it does so obliquely, permitting the south-east
side of the arch to open out towards the south-west, and the north-
west side to expand towards the north-east ; so that we have an
almost complete section between Llangwyllog and Llanerchymedd
as we have between Porth Nobla and Aberfiraw, but with the oppo-
site dip.
The large area occupied by the granitoidite may seem to require
explanation. As this rock rarely exhibits bedding, its relations
are frequently obscure; but, fortunately, in the district between
Gwalchmai and Llechyn farwy the dark Holyhead schist, which
immediately underlies it, is brought up by repeated undulations.
Near Gwalchmai, for example, the granitoid rock dips north-west ;
but to the west 1t is thrown off in opposite directions in the Craig-
yr-allor anticline. The granitoidite is, then, a band of no great
thickness, repeated by contortions. ‘There is also evidence of repe-
tition by faults.
The generalized section (fig. 1) represents the relations of the
principal rock-groups in Anglesey.
LV. NorrHern AREA.
This district is bounded on the south by the curved fault which,
starting from near Carmel’s Point on the west, passes round by way
of Llanfilewin and Paris Mountain to the east coast at Porth-y-
corwg. The rocks are very much contorted and broken; but there
appears to be, on the whole, an ascending series from the fault to the
north coast. The dip is generally to the north; but on the west it
is to the north-east.
1. Volcanic group of Paris Mountain.—The chief types of this
922 C. CALLAWAY ON THE ARCH AN
ridge are a felspathic breccia and a compact felspathic rock like
hornstone; but both varieties are quite distinguishable from any
other rocks in Anglesey. At the east end of the hill, by the Pen-
sarn chapel, the breccia is well exposed. The fragments, some of
which are a yard in diameter, are a very compact felstone; and the
matrix is a sort of greenish ash. The rock, as a whole, reminded
me of the compact breccias at Clegyr Bridge, St. David’s. Prof.
Bonney has since examined a shde; and he is of opinion that it
exhibits both perlitic and fragmental structure and is in all proba-
bility a rhyolitic ash. The dip of the series is to the north, agreeing
with that of the adjoining slaty group. About 100 yards to the east
of the chapel, and therefore on the same strike, is a knoll composed
of a pale-green and purple rock, very compact, almost like jasper.
Under the microscope (Note 53, p. 236) it is seen to be a trachyte,
probably from a lava-flow, and is, in Prof. Bonney’s judgment, as ~
modern in its appearance as the rock composing the enclosed pebbles
near Bodorgan. The purple variety is not unlike some of the fiinty
felstone common in the Precambrian of Shropshire. From litho-
logical characters the Archean age of this group appears not
improbable, though it must be conceded that it does not resemble
very closely the volcanic group south of Bangor. Field work throws
little ight upon the problem. On the north side the ridge is bounded
by afault; and at the base of the southern escarpment black shales
seem to pass conformably under the volcanic group. The two rocks
appear within three or four feet of each other, dipping in the same
direction into the steep face of the hill. There are, however, no
signs of a passage between the black shales and the compact felspa-
thic rock. The appearance of conformity might be produced by
faulting, accompanied or followed by lateral pressure; and there are
abundant proofs of both in the district ; but, under the circumstances,
I hesitate to include this group in the slaty series.
2. Chloritic Schists of Mynydd Mechell.—This group is the “ foli-
ated grit” of Ramsay. In the field it has the appearance of a
quartzose grit, with chlorite covering lamination surfaces ; but Prof.
Bonney, after microscopic examination, regards it as a true schist
(Note 45, p. 234) of the Holyhead type, though he admits that the
chloritic constituent is ‘rather minute.” These rocks are much
contorted, and are frequently penetrated by dykes of felstone and
dolerite running with the strike. At a higher horizon, at Cas
Clock and west of Rhos-y-pill, the rock is an undoubted schist with
silvery lustre (Note 46, p. 234). Some of the strata north-east of
Paris Mountain are not unlike this schist, as may be seen at Cerrig,
on the Amlwch road.
It is important to observe that Prof. Bonney agrees with me in -
recognizing (Notes under C, p. 284) a difference between these
schists and those of the gneissic districts ; but in such a broken
country it is difficult to prove that these rocks should go with the
slaty series. My reasons for so associating them are the following :—
(1) The rocks are not uniformly foliated. To the west of Cas
Clock, for example, chloritic schist is overlain in the same quarry
GEOLOGY OF ANGLESEY. 995
by hard grits. In the same neighbourhood are bands of hornstone,
similar to ordinary Pebidian types, associated with schist.
(2) These rocks appear to pass up through less altered varieties
into slightly metamorphosed grits and shales, as seen south of
Llanfechell and in localities to the east.
(3) The alteration is not carried so far as is usual in the older
series.
(4) In the undoubted siaty districts, as west of Cerrig Ceimwen,
the rock frequently undergoes partial metamorphism, and bands
occur which might almost pass for true foliated schists.
(5) This area is scored with intrusive dykes. I do not suppose
that these are the cause of metamorphism; but they indicate the
proximity of a source of heat, which may have been concerned in
the change.
3. Llanfechell Grits—The altered rocks of Mynydd Mechell appear
to pass to the north into a series of green grits, well exposed round
Llanfechell. This rock has undergone much alteration, to which
probably the colour is due. Microscopic examination (Note 47, p. 234)
brings to light the important result that it is “ almost certainly
derived from the older gneissic and schist rocks of this region of
North Wales.” These grits are also seen on the strike to the south-
east near Bodewryd.
4, Rhosbeirio Shales.—W est of Rhosbeirio church, and in a quarry
near the farm, are very interesting exposures of felspathic rocks of
the true St.-David’s type. These shales are soft, well laminated,
and fine-grained; but here and there are thin seams of grit like the
variety just described. While the body of the rock is but slightly
altered, the gritty bands have a very schistose look. The prevailing
colours are pale green and purple; but there are also some beds of a
soft yellow shale, like a common variety in North-western Anglesey.
The dip is to the north at 30°. Under this group, at Nant-y-cyntin,
slaty beds of a more altered character, intermediate between these
shales and the Cas-Clock schist, are seen.
5. Sharply contorted Group south-cast of Amlwch.—At Crogan
goch and on towards Llaneilian are exposed the remarkable rocks
described and figured by Prof. Ramsay. The foliated structure (Note
49, p. 234) of these slaty-lcoking beds is not very evident to the
naked eye. Similar rocks compose the tongue-shaped promontory
of Point A‘lianus; but sometimes contortion is wanting. At the
base of the promontory the beds are gritty and partially altered
(Note 48, p. 235).
6. Amlwch Slates and Cemmaes Limestones.—South of Amlwch,
near Crogan goch, the last group, with the intervention of an ashy
band, is succeeded by uncontorted pale-green chloritic slaty beds
(Note 50, p. 235), which are continued to the coast and all along the
west side of Bull Bay to Ogo’ goch. The dip is steadily to the
north at a moderate angle; and the thickness must be considerable.
Towards the west, on Porth wen, bands of limestone and quartz-
conglomerate come in; and further west, on Cemmaes Bay, limestone
and quartz rock predominate over the slaty beds. I am not certain
D4 C. CALLAWAY ON THE ARCH.BAN
that the Amlwch and Cemmaes groups are on the same horizon ;
but the evidence appears to point in that direction. The limestone
(Note 52, p. 236) is very similar to a rock at Llanfaethlu; and the
associated slaty beds are alike in both localities; but it would be
rash to correlate the groups.
The northern area (omitting Paris Mountain) is thus seen to
consist of chloritic schists, felspatho-quartzose grits, felspathic shales,
chloritic slates, quartz-conglomerates, and grey limestones, with some
limestone bands on more than one horizon. In such a shattered
district a true succession.can hardly be indicated. North of Paris
Mountain some of the horizons are probably faulted out of sight,
and it is difficult to correlate the rocks of this district with those
further west. Most of the groups appear to pass into each other,
either vertically or laterally ; and I cannot avoid the conclusion that
they all belong to the same epoch.
V. NortH-wESTERN AREA.
In Western Anglesey are two well-marked groups of strata, which
I regard as the equivalents respectively of the Gneissic and Slaty
series. They are brought together by a fault.
Porth-y-defaid Fault.—This dislocation is situated on the west
coast, about midway between the northern and southern extremities.
It 1s well seen on the shore, striking inland to the east. Greenstone
is erupted along the line of junction, and alters the strata for a
short distance on each side. South of the fault are thoroughly crys-
talline quartzo-micaceous and chloritic schists dipping north-west ;
while close at hand on the north side green ashy shales dip north-
east. This fault is the boundary between the two series ; for true
schists with a south-west strike occur everywhere to the south,
while a comparatively unaltered group, with a prevailing northerly
dip, stretches right up to the north-west corner of the island.
Section from the Fault to Pen brywv Eglwys.—Proceeding north-
ward, we find at Trefadog ashy shales dipping north-east. In the
quarries north of Llanfaethlu church is a good section of grey lime-
stone and pale-green ashy slate with easterly dip. The former is com-
pact, and apparently as unaltered as any Paleozoic limestone. A
careful search revealed no trace of fossils. The slaty rock is of a
common Anglesey type; and the whole group is like the Cemmaes
series. About Llanrhyddlad exposures are numerous. At Porth
Swtan, on Church Bay, is a considerable thickness of yellowish fel-
spathic slate and breccia. The dip is north-east, with slight contor-
tion on a small scale. Higher beds are seen in quarries at Rhyd
Ngharad; the rocks are brecciated in part and very felspathic.
Greenish colours predominate. One variety, a pale-green slate,
contains cubic pyrites. On about the same horizon, at Ogo Lowry,
are green brecciated rocks more highly indurated.
The district between Ogo Lowry and Penbryn’r Eglwys is one of
the most faulted parts of the island ; the section consists of alterna-
tions of Archean and Paleozoic rocks, repeated by faults, and dipping
to the north. The wedges of dark shale let in amongst the older
group are very clearly seen in the sea-cliffs. The younger shale, of
GEOLOGY OF ANGLESEY. 225
course, frequently appears to pass under the felspathic series. Such
facts suggest great caution in trusting to dips in areas where the
faulting is not clearly seen. The lithology here, as generally in
Anglesey, is the true guide. The Precambrian chiefly consists of
felspathic breccia. The fragments are usually of similar composition
to the matrix; but some are of quartzite. The felspathic fragments
weather out sharply where the cliffs are washed by the spray. On
the whole this rock strongly suggests the breccia near Nun’s Well,
St. David’s. Good exposures are seen at Yynys y fydllyn, Porth yr
hwch, and west of Pant yr Kglwys. The thickness, owing to such
frequent faulted repetitions, probably is not great.
The section at Pen bryn’r Eglwys is of much interest. In this.
great headland, which juts out at the north-west corner of Anglesey,
are rocks which are described in the section of the Survey Map as
‘‘ oneissic rocks pierced by granite veins ;” and these are represented
as passing on the south into “ metamorphic foliated rocks.” The
latter are the felspathic shales and breccias already noticed. The
description of the former also requires modification.
The breccias pass up into the southern slope of the headland,
where they are succeeded by a band of quartzite. This is over-
lain by a considerable thickness of greenish felspathic beds of ordinary
Pebidian type and not much altered. ‘The highest ridge of the
promontory consists of this rock. Following these strata across the
strike to the north, they are seen gradually to change, the rock
putting on a glazed aspect, and mica appearing in small quantities
on the lamination-planes. This altered material soon passes into
thoroughly foliated gneiss and granitoidite.
It was rather startling to find true metamorphic rocks associated
with comparatively unaltered felspathic beds of the newer series.
The granitoidite is very similar to that of the older gneiss; and my first
impulse was to refer it to that group. In sucha shattered district
as Anglesey, especially in such an area as its north-west corner, a
faulting-up of the older series seemed not unlikely. But, after careful
examination, I found it impossible to accept this supposition. The
‘transition between the unaltered rock and the schists is gradual and
complete. <A close comparison furthermore revealed hthological dis-
tinctions between the gneiss of the two series, the most important
of which is a difference in the colour and lustre of the mica.
The cause of metamorphism was not apparent. The “granite
veins ” of the Survey are probably the granitoid bands in the gneiss.
Some quartz veins running across the cliffs may have suggested the
intrusion of granite. As this metamorphosed mass occurs in the
neighbourhood of the Mynydd-Mechell schists, the alteration in both
cases may be due to the same general cause.
VI. Western AREA.
All the rocks south of the Porth-y-defaid fault and west of the
Paleozoic area belong to the older series.
1. The Mainland.—This district is chiefly occupied by green
chloritic schists (Note 37, p. 234) similar to the rocks described from
the Menai anticline, Aberffraw, Craig yr allor, and east of Paris Moun-
&
226 C. CALLAWAY ON THE ARCHAAN
tain. ‘The dip is usually to the south-east; but the beds frequently
roll over to the north-west, as may be seen south of Porth twyn-
mawr, and at Caer ceiliog on the Holyhead road. There is no doubt
that these schists represent the dark green band which in the
central zone underlies the granitoidite.
2. Holyhead District.—Chloritic schists are well seen at many
points in and round the town. <A typical specimen from Porth felin
(Note 36, p. 234) is of the same character as the schist at Porth y
defaid. The strikeisto thesouth-west; and undulations arenumerous.
These rocks are separated from the quartz group by faults: one, on
the south-west, runs from the south coast, at Porth y corwel, to the
south end of Holyhead Mountain ; and another, on the north-west,
hes along the south-eastern base of the mountain and cuts the coast
at Porth yr Ogof.
Porth-yr-Ogof fault.—Prof. Ramsay * states that the “ quartz
rock” dips under the ‘“ fohated schists ;’ and he gives a section in
support of his opinion. ‘This view would have greatly simplified
my work ; but on visiting the spot I was disappointed to find that the
two groups were brought together by a fault. There was a notch
in the cliff; on one side was quartz rock, and on the other green
schists (Note 35, p. 234), with no signs of a passage. The break
was filled in with fallen rubbish. It was very fortunate that this
dislocation was discovered, as it compelled me to seek the true
succession elsewhere.
Holyhead Mountain.—The microscopic examination (Note 31,
p. 233) of a typical specimen of the quartz rock from the great quarry
shows that it is a true quartz-schist of the same type as the Bodafon,
Gwalchmai, and Mynydd-baen quartz groups. The structure of the
mountain is interesting. Ascending the south-east slope, separation-
planes are seen to dip to the north-west at about 80°; but on the
north-west side the dip changes to south-east at the same angle. The
planes are not close and even, as in slaty cleavage, but they cause
the rock to split in large thick flat flakes. This difference is doubtless
due to the coarseness of the material; and the planes must represent
true cleavage. ‘The cleavage-strike agrees with the strikes of the
contorted bedding and of the ridge.
The Holyhead district is thus brought into clear comparison with
other parts of Anglesey. The chlorite-schists undoubtedly repre-
sent the dark schist which underlies the granitoidite in the central
zone; and the quartz-schists may with the highest probability be
placed on the same horizon as the foliated quartz rocks of Bodafon
and Gwalchmai. The absence of the grey gneiss is easily explained.
On both the west and south the junction between the quartz and
chloritic groups is a fault; but the two formations dip in the same
direction, and the downthrow is apparently on the side of the chlo-
rite-schist. As the latter group is repeated in numerous shallow
curves, there is no reason why the grey gneiss should appear at the
surface, as it does amidst the deeper undulations of the Menai anti-
line.
* Geology of North Wales, p. 185.
4,
GEOLOGY OF ANGLESEY. QF.
The chloritic rocks of this area are rather more quartzose than in
most Anglesey localities; but they resemble some of the varieties in
Mynydd Liwydiarth, and there are indications in both districts
that a source of quartz-derivation was not far distant.
3. Rhoscolyn District.—The south-eastern half of Holyhead Isiand
is similar in structure to the Holyhead area; but the rocks are
affected by an upheaving force to the south, so that the prevailing
dip is to the north. The green schists, which occupy the chief part,
need no further description. ‘The southern fault, which separates
the quartz and chloritic groups south of Holyhead, passes under the
sea, and holds the same relation near Khoscolyn. It is first seen
near Bwa du, and again appears on the coast tothe south-east at Borth
wen, passing in its course near Rhoscolyn church, where the quartz-
schist (No. 32, p. 233) is exposed, dipping northerly. A few yards to
the north the chloritic group dips in the same direction, at about the
same angle. At Bwa du the junction is well seen, both series dip-
ping northerly, the green schist at a lower angle than the other.
The quartz group forms an elevation, Mynydd Rhoscolyn, as is usual
in Anglesey.
At Borth Saint, south of Bwa du, the contortion is intense. There
is evidence, from the folding of quartz veins, that the rock has been
squeezed to one fourth of its original bulk. At one spot there is
a very curious specimen of ripple-mark, distorted so as to be almost
unrecognizable. Quartzite dips to the north, and is underlain by
soft schist. The under surface of the former overhangs, and is
covered with rounded projections, which are evidently the squeezed
easts of ripple-marks. The schist was the mud which received the
impressions of the ripples; and the quartzite represents the sand
which covered in and preserved the marks. I have elsewhere*
figured and described the above phenomenon. It is important to
record ripple-marks in so ancient a formation.
South of the last locality is a considerable thickness of chloritic
quartz-schist (Note 33, p. 233).
B. Summary or REsvutts.
I. Distrrpurion or tHE Rocks.
[See Map (Pl. VIII.) and Fig. 1.]
a. Gneessic Serres.
1. Geographical Distributcon—This series occupies the greater
part of the Menai anticline. It reappears west of the Llangefni
slaty area, and forms the whole of the central zone, except the
faulted mass south-west of Bodafon Mountain. It then reemerges
west of the Paleozoic, and covers Western Anglesey south of the
Porth-y-defaid fault. About three fifths of the area coloured
“‘ altered Cambrian and Silurian” consists of eneissic and schistose
rocks.
* ‘Science for All,’ part xxxi. pp. 205 and 205.
228 C. CALLAWAY ON THE ARCHAAN
The hdlleflinta forms a band extending from Porth Nobla to
near Gwalchmai. It is probably represented north of Llangwyllog.
The quartz-schist extends on the strike from Mynydd baen to
Gwalchmai. It may occur in its place north of Llangwyllog; but
it emerges in the craggy mass of Bodafon Mountain and in the
small inlier to the east. In Western Anglesey it forms the eleva-
tions of Holyhead Mountain and Mynydd Rhoscolyn.
The grey gneiss is brought up through the dark schist on the
western side of the Menai anticline at Gaerwen and east of Pentraeth.
In central Anglesey it runs from near Porth Trecastell to north-
east of Bodwrog, reappearing soon after on the opposite side of the
anticline north of Llangwyllog, and further to the west in the Craig-
yr-allor anticline. ‘To the north-east it is seen in the area south-
east of Paris Mountain.
The dark schist oceupies the greater part of the Menai anticline.
It emerges west of the Llangefni “‘ syncline,” but is gradually faulted
out towards Gwalchmai. On the opposite side of the central anti-
cline it forms a band as far to the north-east as Plas Llanfihangel,
and is brought up through the granitoidite in the oval dome of Craig
yr allor. Italso occurs south-east of Paris Mountain. In Western
Anglesey it constitutes the schistose area south of the Porth-y-defaid
fault and north of the quartzose masses.
The granitoidite is the “ granite” band of the Survey. The details
are inaccurately laid down in their map at many points; but little
theoretical importance attaches to these errors. There are slight
traces of this rock on the west side of the Menai anticline.
2. Stratigraphical Distribution.—One of the most difficult pro-
blems in Anglesey was to make out the succession of the subdivisions
of this group. In no single section, owing to the faulting, is the
series entire; but the subdivisions are recognizable by their litho-
logical characters; and by comparing localities the fragments
are pieced together into a complete succession. The facts will be
best expressed in the following table, the groups being taken in de-
scending order :—
| | |
| j . |
| 1. Holy-| 2. Craig 13. Coed-}4. Dulas} 5. Ty 6. Menai
| : cr ee : Croes, |O- Menai.
head. | yr allor.| ana. Bay. roes.
| |
| Granitoidite ...!... % * | x iy Traces. |
| Dark schist ... * * x * * x ;
Greysomeiss i: mie * x * % * |
Quartz-schist ... x a ? as
Halleflinta ... wee ie ? vee * :
The star indicates the existence of the subdivision in the locality
at the head of the column. By comparing 5 with 2, 3, and 4, it
will be seen that two groups are common to the four areas; and
they serve to link together the lowest and highest subdivisions.
GEOLOGY OF ANGLESEY. 229
The series is probably complete in 3; but in running the section L
could get no exposure between an obscure opening of hiilleflinta and
the grey gneiss, and I had not time to search beyond the highroad.
b. Slaty Series.
This group occupies four areas, viz. the small mass south-
west of Pentraeth, the east side of the Llangefni “syncline,” northern
_ Anglesey, and the western division north of the Porth-y-defaid
fault. The chief facts are thus summarized :—
(1) South west of Pentraeth (Wugan-bach ridge).
Slaty and dolomitic rocks.
(2) Llangefni district.
Slates (some hypometamorphic*), grits, green conglomerates,
purple and green shales, hornstone, calcareous beds.
(3) Northern district.
Chloritic schists, altered grits, green and purple shales, slates
(some hypometamorphic), quartz-conglomerates, limestones,
hornstone.
(4) North-western district.
Yellow felspathic shales and breccias predominating, quartz-
conglomerates, pale-green slates, and limestones.
J am not prepared to submit ascheme of the succession. The rocks
of area | are not unlike some of those near Cerrig Ceimwen in area
2. Comparing 2 and 3, the rocks are similar as a whole; but the
green conglomerate, so conspicuous in 2, is not seen in 3, while the
quartz-conglomerates and grey limestone of 3 do not appear in 2.
Portions of 3 are also altered to schist, while in 2 the transition
into foliated rock is rarely complete. The felspathic breccias of 4
do not certainly occur in any of the other areas; but its quartz-
conglomerates, slates, and limestones are similar to those of 3. The
interesting Rhosbeirio shales in 3 have less complete representatives
n 2, but are fully exhibited in 4.
The rocks of these four areas, though geographically isolated, are
closely connected by their mineral and petrological characters, and
I have no hesitation in placing them all in the same group. Should
the chloritic schists of the north be separated from the newer series,
it will not materially affect my general conclusions. The same
remark applies to the small patch of gneissic rock at Bryn ’r Eglwys.
II. Evipencr or AGE.
a. Relations to Paleozoic Groups.
Gneissic Series.—It is not necessary to recapitulate the evidence
for Precambrian age. The sections in the quarries near Nebo would
alone be sufficient to remove’ all doubt.
Slaty Series—These rocks do not clearly underlie any part of the
Cambrian ; they are, indeed, overlain by a purple conglomerate on
the north coast, west of Tor Ilwyn. The pebbles of this rock are a
* The term “submetamorphic,” used by some authors, is objectionable on
grammatical grounds.
Q.J.G.S. No. 146. age
930 C. CALLAWAY ON THE ARCH EAN
purple quartzo-felspathic grit; but I have no certain proof of its
age.
"The Precambrian age of the series may be inferred from included
fragments. The rocks west of the granitoid zone are shown by the
fossils collected by Prof. Hughes to be Tremadoc and Arenig. In
the conglomerates west of Llanfaelog, which appear to be of at
least equal antiquity, a large proportion of the pebbles are certainly
derived from the Slaty series, pale green and purple hornstone and
slate being the most common. It is also worthy of notice that
the Harlech conglomerates of Caernarvonshire contain fragments
of green and purple slate *, which must therefore be Precambrian
and of no distant source of derivation.
The relations of these series to the Cambrian rocks in contact
indicate the same result. At numerous points the two groups are
brought together by faults; but while the Slaty series is generally
more or less altered, the Cambrian shales are quite unchanged, and
Lhave never observed the slightest indications of a passage betweer
the two, the line of demarcation being always clear and sharp. The
Slaty series must therefore have undergone partial metamorphism
before the Cambrian period, otherwise it is difficult to see how the
Cambrian rocks could have remained unaltered.
The black shales in some localities dip as if they would pass under
the altered series; but at many points the latter also appear to pass
beneath the former. In such a shattered district this evidentey is
worth nothing in either case, unless an “unbroken sequence can be
proved.
I am not prepared absolutely to deny that true Harlech rocks
occur in Anglesey. There are beds, especially near Llangristiolus,
which lithologically do not appear to be. very distinctively Pre-
cambrian ; but, as stratigraphically they are closely associated with
the Slaty series, it is safer to place them in that group.
b. Relations to each other.
In all parts of Anglesey the junction of the two series, whenever
they are in contact, isafault. In the east and centre they generally
strike in the same direction; but in the north-east (near Paris
Mountain), at the base of Bodafon Mountain, and. inthe western
district, as seen north and south of the Porth-y. -defaid fault, the
strikes are discordant, sometimes approaching a right angle. The
much more intense metamorphism of the gneissic series would seem
to point to a greater antiquity. Some additional light is thrown
upon the subject by the microscope. Prof. Bonney, in note 47 (p. 234),
already noticed, is decidedly of opinion that the Llanfechell grit, a
characteristic variety of the newer rocks, is derived from the older
series.
c. Relations to other Areas.
(1) Caernarvonshire.
Comparing the Slaty series with the Bangor group, the re~
* Bonney, Quart. Journ. Geol. Soc. vol. xxxv. p. 511.
GEOLOGY OF ANGLESEY. 31.
semblance, it must be confessed, is not very close. Both formations
are largely of volcanic origin; but the felspathic materials of the
Anglesey rocks are derived from a more distant source, while the
frequency of quartzite pebbles indicates the proximity of land not
covered by volcanic products.
The Gneissic series would appear to be closely related to the
granitoid rock of Twt Hill. As the normal position of the dark
schists is below the granitoidite, there seems to be no reason to
doubt that the green schists on the Anglesey side of the Menai
Straits pass conformably beneath the Twt-Hill beds. The post-
Carboniferous fault on the west side of the T’wt-Hill ridge might
not materially affect the true relations of the older subdivisions.
(2) St. David's.
_ Slaty Series.—The lithological resemblances between this group
and the St. David’s Pebidian are numerous and striking. The
varieties whose Pebidian facies is most marked are the pale-
green, purple, and yellow felspathic shales of Rhosbeirio, the
felspathic breccias north of Llanrhyddlad and east of Bodorgan
station, the tough green rock at Cerrig Ceinwen and Cerrig-engan
fawr, porcellanitic bands near Llangristiolus, and hornstones of
many localities. The slaty beds are less distinctively of St. David’s
type.
Fe ncicsic Series—The Anglesey granitoidite has been compared
by Messrs. Bonney and Hicks with the St. David’s Dimetian. If
this correlation be conceded, the entire Anglesey series, from the
hilleflinta upwards, must go with the Dimetian. But it must be
admitted that the two.groups present important differences. At St.
David’s the Dimetian is represented by a great thickness of grani-
toidite and quartzite ; whereas in Anglesey the similar band is much
thinner, and is underlain by a considerable thickness of gneiss and
other schists.
(5) Shropshire.
The felspathic slaty beds of Lileshall Hill are hardly distin-
guishable from some of the Anglesey rocks. The Lilleshall group
is probably higher than the Wrekin volcanic rocks, which have
many points of resemblance to the fragmenta! group south of Bangor.
The purplish ash of the Wrekin, for example, is very similar to the
srit at Bryn Ilwyd. Nothing certain, of course, can be inferred
from such facts; but it is at least worthy of consideration, and the
suggestion may be a guide in further inquiry, whether the Anglesey
Pebidian may not represent a higher horizon than the Bangor group.
Some of the gritty and slaty rocks of the Precambrian ridges east
of Church Stretton also display affinities with the Anglesey series.
It is worthy of note that the Charlton-Hill conglomerate, an
undoubted part of the Wrekin group, contains, amongst enclosures
from the Malvern series, pebbles of rocks which more closely
resemble some of the gneissic and quartzose types of Anglesey.
k2
232, PROF, T. G. BONNEY ON THE MICROSCOPIC
(4) Charnwood.
The slaty rocks of Anglesey are nearer in their lithological
characters to the Charnwood slates than to any other formation with
which I am acquainted. The resemblance was very marked even
in the field ; but in the case of a homogeneous rock like slate, the
microscope is of special value, and Prof. Bonney’s examinations
(Notes 42, 43, 44, pp. 234, 235) are strongly confirmatory of my
opinion.
CoNCLUSIONS.
1. In Anglesey there are two Archean groups, the Slaty and the
Gneissic.
2, The Slaty series is composed of slates, shales, hornstones, grits,
conglomerates, limestones, and chloritic schists, in which no definite
order has been positively ascertained. The Gneissic series is divided
into five groups, in which the following descending order is in-
variable, viz. granitoidite, chloritic and hornblendic schists, grey
gneiss, quartz-schist, and hilleflinta.
3. The Slaty series is occasionally foliated, but is usually in a
partially altered state: the Gneissic group is thoroughly meta-
morphosed.
4, The Slaty series has closer lithological affinities with the St.-
David’s voleanic group, the Charnwood rocks, and the Lilleshall
series than with the Bangor group.
5. The Slaty series is undoubtedly Pebidian: the Gneissic series
may with some probability be referred to the Dimetian.
APPENDIX.
Notes on the Microscopic Structure of some ANGLESEY Rocks.
By Prof. T. G. Bonnny, M.A., F.R.S., Sec. G.S.
In the following notes I shall endeavour to avoid repetition by
grouping together those specimens which in some important cha-
racteristics have a general resemblance one to another. I may
add that, as the purpose of my examination was petrological rather
than mineralogical, I have not felt bound to spend. much time in
endeavouring to ascertain the exact species of some microlithic
minerals which are accidentally present in one or two of the slides.
A. Quartz-Schist Group.
Nos. 25-29, 31-34.
This group consists of a series of schistose rocks, in general highly
metamorphosed, in which quartz is the most important constituent,
associated with micaceous or chloritic minerals, ferrite or opacite,
and more or less felspar.
The fragmental origin of most of these specimens is indubitable ;
but with regard to numbers 25 and 27 it is less easy to be quite
sure. Their structure comes nearer to that of some microcrystal-
line felsites ; but still I believe that I am right in ranking these also
among the altered clastic rocks.
25. (Gwalchmai, p. 218.) Contains numerous grains of quartz of
STRUCTURE OF SOME ANGLESEY ROCKS. 233
rather irregular outline in a finely granular and rather earthy-looking
matrix—most probably the result, in the main, of the decomposition
of rather imperfectly crystallized felspar, which consists now of
an admixture of earthy dust, doubly refracting clear microliths,
and minute scales of mica or chlorite. The quartz grains show
an indistinct banded order, and contain many minute cavities. The
rock appears to have been brecciated more than once zn situ. The
older cracks are mainly filled up by quartz, the newer by calcite
with a little chlorite. In one part of the slide the faulting of an
older vein and subsequent infiltration of a newer one is very
clearly shown. Macroscopically the rock has aresemblance to the
Treffgarn halleflinta, but under the microscope it is more gneissic.
26. (Gwalchmai, p.218.) Is certainly of fragmental origin, show-
ing stratification foliation. The quartz grains have fewer inclusions;
there is felspar much as before, and a fair quantity of mica; most of
this is of a very pale golden-yellow colour, is feebly dichroic, and
gives brilliant tints between the Nicols; the rest is dull green,
probably an alteration produced after biotite. Some granular matter
as above.
27. (N.W. of Gwalchmai, p. 218.) More resembles 25, but is more
compact. I think that it, too, is of fragmental origin, and is pro-
bably the result of the metamorphosis of a fine quartzose silt.
28. (N.W. of Gwalchmai, p. 218.) Is certainly fragmental, con-
sisting of quartz with a fair amount of chlorite, some white mica,
and a few grains (probably fragmental) of a closely twinned plagio-
clastic felspar.
29. (Summit of Bodafon Mountain, p. 219.) Is a quartz-schist
with a fair amount of ferrite and minute chlorite (?).
31. (Holyhead Mountain, p. 226.) Also a quartz-schist with a fair
amount of a pale-green mi¢a, as above, the ground-mass consisting of
this mineral with agglutinated very minute grains of quartz. In this
are scattered quartz grains of larger size up to about 003 diameter,
clearly of fragmental origin, some having a secondary deposit of
quartz on their edges. Minute cavities are common in these grains,
and one or two contain some dark hair-like microliths, a grain or two
of epidote, and possibly one of tourmaline.
32. (Rhoscolyn church, p. 227.) Also a quartz-schist resembling
the last, but more uniform in structure; the same adventitious
minerals as in the last.
33. (S. of Borth Saint, p. 227.) Another quartz-schist with rather
more mica and chlorite, a few grains of felspar, and the same adven-
titious minerals. Numerous grains of a granular earthy mineral
(? an epidote).
34. (Cutting EK. of Ty Croes, p. 217.) Quartz and a while mica
are the most conspicuous minerals, with an occasional grain of
felspar; but a sort of granular paste in which these are imbedded,
consisting of microliths of white mica and other minerals, may in
some cases have replaced a felspar constituent. The rock is much
altered, but, I suspect, still retains in its large grains traces of its
original fragmental structure.
234 PROF, T. G. BONNEY ON THE MICROSCOPIC
B. Chlorite-Schists.
A group of highly altered, distinctly foliated rocks, consisting
mainly of rather minutely crystalline chlorite and quartz. To this
belong Nos. 35-37, 45, 46, 49.
35. (Porth yr Ogof, Holyhead, p. 226.) Contains very numerous
rods and granules of a black mineral, perhaps magnetite, with a little
sphene or staurolite; it exhibits beautiful contortions.
36. (Porth felin, Holyhead, p. 226.) Foliation less marked ; a con-
siderable amount of ferrite is present. Original structure perhaps
less uniform than in the last.
37. (Porth y defaid, p.225.) The same remark applies to this speci-
men also, but itsfoliation is moremarked. A vein of quartz and calcite.
rather minute.
46. (Cas Clock, p. 222.) Highly altered and markedly foliated.
49, (Crogan goch, p. 223.) The same; chloritic or possibly mica-
ceous constituent extremely minute; beautifully foliated and contorted.
In this group, as a rule, it is more difficult to identify with
probability any original constituent of the rock, owing probably to
differences in chemical composition and size of the materials. Some
of the quartz grains in 37, 45, 46 may, however, be original.
C. Slaty and other not highly altered Rocks.
In this group there has, indeed, been a certain amount of altera-
tion, but it is only what may be termed micromineralogical. The
original fragmental character of the rock is still distinct ; the newer
products are either extremely minute or such as result rather from
decomposition than from recomposition. The alteration, in short, is
of a kind which we commonly meet with in the earlier Cambrian or
latest Precambrian rocks, not in the gneisses, in the conspicuously
foliated schists, and in the most highly metamorphosed quartzites. Its
members, then, are, as a rule, either much more modern than those
previously described, or selective metamorphism must have operated
upon the latter to a rather unusual extent.
43. (S.E. of Cerrig ddwyffordd, pp. 214, 232.) One of the flinty
argillites or indurated imperfectly cleaved slates. Under the micro-
scope the slide consists of a brownish-grey earthy-looking material
interspersed with minute specks of quartz, felspar, and micaceous or
chloritic minerals, whether original constituents or of secondary origin
it is in many cases difficult to say. The “stripe,” however, is well
indicated, and the specimen in no important respect differs from
many examples that I have examined from Charnwood and other
localities where the rocks are approximately of Cambrian age.
44, (W.S.W. of Cerrig Ceinwen, pp. 215, 232.) A similar rock
of slightly coarser material and a little more distinctly cleaved.
Among the constituents are many scales of a strongly dichroic green
mineral with a marked wavy cleavage—chlorite or some member
of the provisional viridite group, probably the result of alteration
of a magnesia-iron mica fragmentally present.
47. (Llanfechell, p. 223.) A coarser fragmental rock with a rather
STRUCTURE OF SOME ANGLESEY ROCKS. 239
«streaky ” structure, not unlike some of those which occur in the
Borrowdale series, containing numerous microliths of the viridite
group, some being certainly chlorite. The aspect of the rock suggests
that it has undergone considerable pressure. Many of the imbedded
fragments are from about 0:03 to 0-06 in longer diameter. Among
them quartz, felspar, altered biotite (?), and a chloritic quartz-schist
may be recognized, detrital materials almost certainly derived from
the older gneissic and schist rocks of this region of North Wales.
Other fragments of a less certain character are present, with grains
of decomposed ilmenite or magnetite and of epidote, which perhaps
has replaced some other mineral.
A8. (Base of Point Athanus, p. 223.) A rock of a generally similar
character ; but, as the fragments are smaller, their nature (except in
the case of the quartz) is less easily ascertained ; the whole rock also
seems slightly more altered than in the last case.
50. (Coast N.W. of Amlwch, p. 223.) The materials are more
homogeneous than in the other cases; small greyish clustered
eranules frequent, and a vast number of microliths of a green
mineral (chlorite?). These are very likely of secondary origin, but
I consider the rock a true slate, and not a schist.
AD, (S.E. of Cerrig ddwyffordd, p. 214.) A fine grit with much
of the fibrous green (? hornblendic) mineral which I have often ob-
served in the Charnwood rocks developed among the finer materials;
the larger fragments (generally rather angular) are chiefly quartz,
felspar (orthoclase and plagioclase), and a minutely microcrystalline
or cryptocrystalline rock, much resembling bits of an acid lava.
From certain minute peculiarities, I have strong suspicions that all
three of these constituents have been derived from rocks of volcanic
origin.
38. (Fragment in Llangefni conglomerate, p. 214.) A grit, consist-
ing of subangular and rolled grains, mostly quartz, in a fine quartzose
or quartzo-felspathic matrix. It is difficult in the case of rocks of this
character to draw an inference as to their age and amount of meta-
morphism; but I believe that I am right in grouping it Tae the
probably more modern series.
D. Granitoid Gneiss.
Of this rock there is one specimen from Pen Bryn yr KEglwys not
at all in a favourable condition for microscopic examination. It
resembles the group of coarse granitoid gneisses similar to those
which I have examined from the neighbourhood of Llanfaelog
rather than a true igneous rock. It consists of quartz with many
minute enclosures, two felspars much decomposed, and various
alteration-products probably replacing an iron-magnesia mica. One
or two grains of another mineral are present, obviously much
altered, which I cannot identify; possibly it may have been garnet.
KK. Crystalline Limestones.
40, (H.N.E. of Tan y graig, Pentraeth, p. 213.) A finally granular
clear rock consisting almost wholly of calcite or dolomite. Judg-
236 PROF, T. G, BONNEY ON THE MICROSCOPIC
ing from the structure and optical characters, I should infer the
presence of a considerable quantity of the latter mineral, and so
name the rock a dolomite.
51. (E. of Bodwrog, p. 218.) Is more coarsely crystalline with an
admixture of quartz grains and some silicate, which I am unable to
identify with certainty ; the carbonate, however, appears tc be mainly
calcite.
Al, (At “a” of “ Pentraeth,” p. 213.) To the unaided eye appears
less crystalline and less pure, resembling some limestones which have
an admixture of volcanic mud. Under the microscope the calcite
appears in rather irregular grains of fair size and rather brecciated
aspect, imbedded in a streaky-looking paste composed of a pale green
serpentinous mineral, of black and dark brown dust, with a little
quartz, and of a clear silicate in minute granules, probably some
kind of zeolite.
52. (Tau isa, N.H. of Cemmaes, p. 224.) Is moderately clear,
chiefly composed of very minute granules of crystalline calcite and
possibly dolomite, with occasional brown stains, and veined irre-
eularly with more coarsely crystalline calcite. In no one specimen
can I detect any distinct trace of an organism; but the first two
rocks differ much from the last two, which might readily pass for
members of the Carboniferous Limestone series.
F, Igneous Rocks.
39. (Fragment in green shale, EK. of Bodorgan station, p. 214.) The
ground-mass is thickly crowded with small and not very sharply
defined felspar crystals, which, in their elongated form and the
twinning of larger specimens, generally resemble members of the
plagioclase group, interspersed with numerous minute grains of a
pale green colour, of which the larger are distinctly dichroic and are
probably hornblende. Small grains and occasional rod-like micro-
liths of an iron peroxide are also present. Scattered about in the
ground-mass are roundish patches of tessellated aspect, chiefly
composed of crystalline quartz; one, in which the crystals are larger
and by their enclosures indicate lines of growth, has calcite at the
centre; this, however, as in the case of a neighbouring vein, is
probably a subsequent infiltration. The majority more resemble
imperfectly formed spherulites; a portion of the slide shows a
distinct fluidal structure, and the ground-mass has a general resem-
blance to several modern lavas, ¢. g. to specimens in my collection
from Astroni and the Solfatara (Phlegrzean Fields).
53. (Carreg-winllan, Pensarn, 8.H.of Amlwch, p. 222.) Exhibits a
rather clear base, in which numerous small roundish patches are
defined by exceedingly minute opacite and ferrite, the latter some-
times forming the inner edge of the boundary ; it is also more or less
powdered about through the base. With crossing Nicols this last is
seen to be crowded with rather acicular felspar microliths, and the
majority of the patches are well-defined spherulites with the usual
radial structure. The rock is undoubtedly a trachyte, like the
other; and, I think it highly probable that each is from a lava-flow.
STRUCTURE OF SOME ANGLESEY ROCKS. Dis ff
Considering the locality and the consequent age of these specimens,
their structure is most interesting. So far as my experience goes,
there is nothing in either which would have awakened my sus-
picions as to their age, had they been labelled as from some locality
where Tertiary or even more recent trachytes are found.
EXPLANATION OF PLATE VIII.
. Map of Anglesey, showing the distribution of the Paleozoic, Pebidian,
and Gneissic series.
. Generalized section from Holyhead Mountain to Menai Straits.
. Section across Mynydd Liwydiarth.
. Section from Porth Nobla to Aberffraw.
- Section in Upper Quarry, Nebo.
. Section in Lower Quarry, Nebo.
In all the sections the signification of the letters is as follows :~-
d. Carboniferous.
c. Cambrian.
BG Pebidian.
,- Granitoidite.
;- Dark schist.
a, . Grey gneiss.
Limestone.
Quartz schist.
. Halleflinta.
. Faults.
Fig.
o> Or 09 bO am
2,8
“We Ny v2
|
_ a, Gneissic series ja
|
|
a,
Q.8
Discussion.
Dr. Hicks agreed with Dr. Callaway that there are two Pre-
cambrian series in Anglesey. He differed from the author, how-
ever, in regarding the so-called granitoidite as constituting the
lowest and not the highest member of the so-called Gneiss
series. He stated that some of the breccias associated with the
halleflintas contain pebbles of the granitoid rocks, and are therefore
of younger age than the latter. He admitted, however, that some
of the points must be regarded as in an unsettled state, owing to
the faulted condition of the district.
Prof. Ramsay argued against the principle of identifying rocks as
of different ages by their mineral characters as studied by the micro-
scope. He maintained that the altered rocks of Anglesey are the
metamorphosed representatives of the Cambrian, because the un-
altered Cambrian are found striking directly towards the altered
strata, and both are overlain by the Arenig.
Mr. W. W. Smyrtu also argued against the recognition of a number
of different formations on mineral evidence alone without any aid
from organic remains. He thought the so-called “ gneissose rocks ”
differ widely from typical gneisses, and that the granitic series
belonged to the class of ill-defined granite rocks known in Corn-
wall as “bastard granite,” the plain Saxon of which was perhaps
preferable to the cacophony of “ granitoidite.” He thought that the
evidence brought forward was insufficient to upset the detailed map
of the Survey.
Prof. Bonnzy was inclined to agree with Dr. Callaway’s interpre-
238 ON THE GEOLOGY OF ANGLESEY.
tation rather than that of Dr. Hicks, as the latter undervalued the
amount of metamorphism the Anglesey rocks by the Menai Straits
had undergone. He differed from Prof. Ramsay as to the value
to be attached to the microscopic study of rocks; he did not regard
the Bangor rocks as partially metamorphosed, and he found no
trace of the progressive metamorphism insisted on by Prof. Ramsay.
He defended the use of the term “ granitoidite,” which, though
open to objections, was less misleading than the base-born term
proposed by Mr. Smyth. He thought that the microscopic study of
the rocks supported Dr. Callaway’s conclusions.
Dr. Cattaway agreed with Prof. Ramsay as to the great value of
the Survey work. He contended that the principle of the identi-
fication of rocks by their mineral characters is a safe one when
applied in the same district. The sections described proved that the
granitoidite was the summit of the gneissic series. Many of the
gneissose rocks were true gneiss of very typical character. The
difficulty through faulting was counteracted by comparing areas.
ON THE LIMESTONE OF DURNESS AND ASSYNT, 239
16. The Limzstone of Durnuss and Assynr. By C. Cattaway, Esq.,
M.A., D.Sc, F.G.S. (Read January 5, 1881.)
Iv is well known that the late Sir R. I. Murchison based his deter-
mination of the Ordovician (Lower Silurian) age of the greater part
of the Scottish highlands upon the discovery by Mr. C. Peach of
Ordovician fossils in the Durness limestone. The views of Mur-
chison were shared by many distinguished geologists, and have been
generally accepted as one of the most assured and important conclu-
sions of modern geological science. Wishing to ascertain for myself
the truth of this opinion, I devoted a portion of last summer to the
study of the limestone at Durness and Inchnadamff. I selected these
localities because they alone are alleged to have yielded fossils from
the limestone, and because Murchison regarded them as of primary
importance in the construction of his argument. My researches led
me to the conclusion, not only that the sections were broken, and
therefore untrustworthy, but that the relations of the several rock-
groups were inconsistent with the supposition that the limestone
passed below any part of the newer metamorphic series. On my
return from Sutherland, I found that many of my observations
agreed very closely with those of Prof. Nicol; and I am glad to
bear testimony to the accuracy of an author whose work has hardly
received due recognition. It is certain that he made out many im-
portant points which escaped the observation of his distinguished
rival; and I must, in candour, acknowledge that he has anticipated
many of the results which I have now to submit to the Society.
I can only claim to have ascertained some additional facts, which
seem to me to strengthen the case against the received opinion.
DuRNEss.
a. The Limestone in Relation to the Flagqqy Gnevss.—In his later
papers, Murchison admitted that the limestone was separated from
the flaggy beds* by a “ great fault,” by which the “ upper quartzite ”’
was thrown down out of sight; but he, notwithstanding, held that
the limestone was ‘“ overlain by the upper series of quartzose and
gneissic rocks,” apparently on the ground that both dipped in the
same direction, to the east. Admitting his facts, his reasoning is
obviously fallacious, and might be employed to prove the most op-
posite conclusions. But I cannot accept his facts. Neither the
limestone nor the flagey group dips to the east. The true relations
of the two formations are shown in the annexed plan (fig. 1), which
is, in outline, a reduced copy of the new ordnance map. The most
important dips are shown by arrows.
* These flags are a true schist, though they are far less coarsely crystalline
than the Lewisian.
240 C. CALLAWAY ON THE LIMESTONE
Fig. 1.—Sketch Map of the Durness Area.
(Scale, about ? inch to 1 mile.)
Mh.
vy NW “ h ‘ B
WwW WNW ees CET TTN
== lauartaite. ie
Koiitis Flagey Gneiss. Limestone. EEE] Blown Sand. f. Faults.
The fault f#, runs from sea to sea, east and west, exactly at the
base of Far-out Head, which is entirely composed of thin-bedded
gneiss and quartz-schist, dipping steadily to the north-east, except
at some points a mile north of the fault, where the dip is conse-
quently unimportant.
West of the ruined church, where the limestone contains numerous
fossils, the dip is north-east, so that 1t might seem as if it passed
beneath the schist. But here the nearest exposure of the latter is
over half a mile to the north-east, the intervening area being occu-
pied by blown sand, so that no junction can be seen. Further ex-
amination proves that this dip of the limestone is exceptional.
Following the strike of the schist to the south-east, we trace it
right up to the fault. Both rocks are here clearly exposed, the flags
on the shore and in the adjoining field, and the limestone in a low
cliff, which is an inland extension to the west of the precipice of
Creag Chearbach. The fault runs along the base of the cliff. The
flags dip uniformly to the north-east, the nearest section being only
twenty yards from the limestone, which, at this point, dips east-
|
22 S8050- Bay Gneiss.
OF DURNESS AND ASSYNT, Q41
south-east. Several dips taken in this locality were the same, others
veered round to the east, but none to the north of east.
Following the cliff along to the west, and noting the prevalenco
of south-easterly dips, we come, at about two furlongs east of Baile-
nacille, to a small arch of limestone, with dips ranging from south-
east to north-east. Such local variations are obviously unimpor-
tant. In the area south of the fault the dips are almost uniformly
to the south-east, as may be seen at many points between the inn
and Sangomor.
Coming back to the west of the old church at Bailenacille, we find
the north-east dip soon changes to east, and then to east-south-east,
and on the Kyle of Durness the limestone forms an escarpment over
a mile long, striking south-south-west and dipping clearly to the
east-south-east. At many other points in the area round Durness
the same dip is seen.
It is then certain that the mass of limestone lying south of the
flags, and in immediate contact with them, dips south of east,
northerly dips being quite exceptional, and then occurring only at a
distance from the schist. As the latter dips steadily to the north-
east, it is difficult to see how it can be conformable to the limestone.
But a more comprehensive view of the district presents the re-
ceived view in a still more incredible light. East of Sango Bay is
the Smoo mass of limestone. Though separated from the Durness
area by a faulted strip of gneiss, it preserves the same south-south-
west strike. Hast of Sangomor it steadily dips east-south-east, at
Smoo it is about horizontal, but west of Sangobeag it turns up to
the south-east and a syncline is formed. On the promontory of
Leirinmohr some of the dips are nearer south than east; but in no
case have I observed in the Smoo mass the north-easterly dip of the
altered series. :
As Murchison himself admits that higher up the valley the
limestone is faulted against the old gneiss on both sides, it is need-
less to follow it further.
b. Geiss of Sango Bay.—Between the two limestone areas is a
band of schist. On the shore it is well exposed, not ‘“ thrust about
in dire confusion,” but forming a symmetrical half-dome facing to
the north-east. On the east side, within a few yards of the lime-
stone, and dipping towards it obliquely (that is, to east-north-east,
at 40°), is hornblendic and chloritic gneiss. ‘Towards the west the
dip curves gradually round to north-east and north, and the gneiss
is then underlain by dark mica-schist, which soon occupies the
shore, the dip turning round to north-north-west, and finally to
north-west, as if it would pass beneath the limestone which crops
up in the shore close at hand, and is seen in the cliffs with its usual
low south-easterly dip. There is no doubt that this strip is faulted
(f, and f,) against the limestone on both sides.
his gneiss is of the same kind as that which underlies the flagey
schist on Far-out Head and east of Loch Hrriboll, and it must not
be confounded with the Lewisian, which in this district is very
massive, coarsely crystalline, and almost vertical inits dip. Accord-
242 C. CALLAWAY ON THE LIMESTONE
ing to received views, this newer gneiss must overlie the limestone ;
and, if so, the force which contorted the former must also have
affected the latter. But though the limestone comes up to the
gneiss on both sides, its gentle south-east dip is not changed. It
would appear to be more reasonable to infer that the limestone was
deposited on the contorted gneiss, and that the latter was subse-
quently thrust up through the former between two parallel faults.
c. The Quartzite——The bay between the limestone promontory
of Leirinmohr on the west and the headland of Lewisian gneiss on
the east is occupied by the quartzite, which is also seen sloping
down from the fianks of Ben Keannabin to the bay and forms a
small outlier on the headland just named. It dips uniformly to the
north-east. In the western angle of the bay it is faulted ( f,) against
the limestone. Both limestone and quartzite are crushed into thick
breccias at the junction, and on the bank immediately above the
limestone is seen dipping to the north-west, the strikes of the two
formations being, as in the former case, nearly at right angles.
To sum up these results, it is clear that the metamorphic rocks,
quartzite and schist, have been affected by a force tilting them up
to the north-east, while the limestone forms a syncline whose axis
strikes to the south-south-west. How the limestone can hold a
conformable relation to the altered groups is a problem which the
advocates of the received view may fairly be called upon to solve.
Though the metamorphic rocks occur in three distinct patches, it
is probable that they form a true succession. To the east of Loch
Kirriboll, the quartzite is overlain by gneiss of the Sango-Bay type,
which is surmounted by the flaggy group on Loch Hope. In Durness
the Sango-Bay gneiss must overlie the quartzite, since the latter
rests on the Lewisian gneiss; and if the flags of Far-out Head were
~ prolonged on the strike to the south-east, they would overlie the
newer gneiss.
ASSYNT.
The section on which Murchison placed chief reliance is the suc-
cession on the south-west slope of Cnoc an drein, above the church.
As I entirely differ in my reading, I submit a section of the ground
(fig. 2), in which I have carefully excluded hypothesis and have
simply inserted the facts observed.
Fig. 2.—Section above Inchnadamff Church.
S.W. ) NE.
L. Limestone. DL. Dark Limestone. F. Felsite.
WL. White Limestone. Q. Quartzite. 7. Fault.
— a ee
OF DURNESS AND ASSYNT. 943
Just above the road we come to a band of dark limestone, which
is succeeded by a white zone. Beyond a little hollow, quartzose
flags are followed by similar dark and white limestones, which are
probably a repetition; then in succession we have felsite, lime-
stone, and felsite. Hitherto the dip of the bedded rocks has been
to the north-east. Above the felsite is a considerable thickness of
quartzite dipping east, so that if it overlies the limestone it must be
unconformable. Higher up the quartz-rock dips for some distance
to the south-west. Approaching the summit of the hill, felsite
appears, and just beyond is massive quartzite dipping steadily to the
south-east for a considerable distance.
It is obviously unsafe to base a succession upon such a broken
section as this. Passing over the intrusions, it is certain that more’
than one fault * occurs, and that the strike of the limestone is at
right angles to the main mass of the quartzite. But a still more
decisive refutation of Murchison’s views remains.
Following the strike to the south-east it is seen gradually to
recede from the quartzite ridge, while opposite dips by degrees come
in on the northern side of the limestone band, which thus expands
in the plateau of Stronchrubie into a broad syncline, the northern
side of which dips away from the quartzite, that is, to the south-
west. Towards the ridge the limestone dips grow steeper and aft
last approach the vertical. Climbing the face of the mountain
above, the quartzite is seen to dip to the north of east, so that the
dips of the two formations are in opposite directions. As the
northern side of the syncline gradually disappears towards Cnoc an
drein, it is obvious that it is cut out by a fault, so that the southern
side of the basin is brought against the quartzite and appears to dip
below it. ‘These facts are illustrated in fig. 3.
Fig. 3.—Plan of Limestone and Quartzite at Inchnadamff.
wy AN
Ca ae
* Almost certain at F, and F,.
244 C. CALLAWAY ON THE LIMESTONE
There is another difficulty in the reception of the old view.
According to Murchison, the limestone is conformably overlain by
the great mass of quartz-rock which rises into the lofty peaks of
Ben More. If so, then the limestone basin of Stronchrubie must
have been covered by an equal thickness of quartzite. It is for the
followers of Murchison to show how denudation could have cleared
off the entire mass of such an intractable rock as quartzite from the
limestone, and yet have made so little impression upon the mountain-
ridges which overhang.
The quartzite which slopes down from the south-easterm face of
Queenaig passes up through a continuous quartzite ridge into Ben
More. It is not pretended that the limestone occurs in this line of
section; but it is very singular that it should have thinned out
just where its presence would have been of decisive value.
One important and suggestive fact remains. At both Durness and
. Assynt the limestone forms a symmetrical basin, the axis of which
does not agree with the normal strike of the rocks which are sup-
posed to overlie, but which coincides with the axis of the existing
valley in which vt les. In Assynt the axes strike to the south-east,
at Durness to the south-south-west.
I do not at present press these conclusions beyond the districts
observed, but submit them as an instalment towards the solution of
a great question.
Discussion.
The PrestpEnt said he had twice visited the area, and felt diffi-
culties in tracing the succession of the rocks, especially as to the
asserted recurrence of the quartzites. The fossils proved the lime-
stone to be of about Arenig age; certainly the limestones seemed
to lie in a synclinal basin on the quartzites.
Prof. Jupp said that, after several visits to the district, he felt
great difficulty in offering an opinion as to the succession of beds ;
he thought the simple sections commonly drawn to illustrate the
geology of the country did not hold good. He considered that
Prof. Nicol had made good his position as to there being only one
quartzite and one limestone; but as to the relation of these to the
gneiss, there was great difficulty in arriving at a satisfactory con-
clusion.
Dr. Hicxs agreed that the limestone series sometimes lay in
synclinal folds of the quartzite; but he thought there might be two
quartzites, as in a case he had recently noticed in another region
along the same line further south. He was thoroughly satisfied that
the series was newer than, and did not underlie, the eastern gneiss.
Mr. Huptrston observed that Dr. Callaway’s mapping of the
Durness area coincided with Sir R. Murchison’s section as to the
limestone being troughed, and also as to the reversed position of
the two gneisses. Further south the quartzites and limestones ap-
peared to be intercalated, as at Loch Erriboll, where Orthoceras had
OF DURNESS AND ASSYNT. 245
been obtained from the quartzite, tending to show that the two
rocks hang together. The Assynt series, though less distinct than
that at Loch Erriboll, was not inconsistent with such an idea. The
unequal tension of the two rocks might in part account for local
discordance of strike.
Dr. Cattaway could not agree with Mr. Hudleston as to his
interpretation of the Durness section; such discordant strikes were
incompatible with the idea of a conformable succession ; nor did
he agree with his view of the Loch-Erriboll rock. He accepted the
age of the limestone,
Q.J.G.8. No. 146. S
246 R. ETHERIDGE ON A TRIGONIA FROM THE
17. On a New Srrcizs of Triconta from the Purseck Bens of the
Vatz of Warpour. By R. Erazripes, Ksq., F.R.S., Pres. G.S.
With a Note on the Strata, by the Ruv. W. R. AnpREws,
M.A. (Read December 15, 1880).
Earty in this year the Rev. W. R. Andrews, of Teffont Rectory,
near Salisbury, placed in my hands what at first sight appeared to
be a new species of Z’regonia from the Purbeck rocks in the Vale of
Wardour. This new species was found by Mr. Andrews in the rail-
way-cutting one mile west of Dinton Station in the Vale of Wardour ;
and its geological or stratigraphical horizon is the “ Cinderbed ” so
well known in the several sections in the Isle of Purbeck and else-
where. This bed is here composed of hard grey marl and pale
brown soft limestones, variable in their proportions. Ostrea distorta
and casts of TZrzgonca abound in this Cinderbed, which here measures
about 2 ft. 6 in. in thickness. The section accompanying this
paper (fig. 2, p. 252) was constructed by Mr. Andrews, and most
correctly represents the succession of the Lower and Middle Pur-
becks at the spot in the vale whence the new Trigonza came. It
was from this marine “‘Cinderbed ” at Durlston Bay that Hemicdaris
purbeckensis, Forbes, was obtained, associated with Ostrea distorta,
a Trigonia like 7’. gibbosa, Cardium Gubbsir, Perna sp., and remains
of fish. No other locality or section of the Dorsetshire Purbecks
has yielded the above. ‘There cannot be any doubt that this 7ri-
goma is not T. gibbosa. The Rev. O. Fisher obtained T'rigonia gib-
bosa(?) from the middle Cinderbed of Fovant, Wilts; and the Rey. Mr.
Andrews has obtained four other specimens of the same species from
his immediate area; so that the genus is well represented in the
Middle Purbeck of the Vale of Wardour. The Lower Purbeck beds
of the vale lie below the datum of the railway and the level at
which many of the quarries are worked, the “‘ Juxeat ” beds being
about the lowest seen. The beds exposed in the railway-section near
Teffont include the base of the Wealden, all the Middle Purbecks of
the Vale of Wardour, and the top of the Lower Purbecks. The middle
group here is about the same thickness as the beds in the Isle of —
Purbeck ; those at Ridgway Hill and Mewps Bay are about 50 ft. ;
and at Worborrow Bay the middle series measures 90 ft., and at
Durlston Bay 150 ft. There is no Upper Purbeck in the area
under observation ; the hard marl with eroded surface is the highest
member of the Middle Purbeck, the succeeding 17 ft. being probably
Hastings Sand at the base of the Wealden.
Description.
Section Glabree.
TRIGONIA DENSINODA, Ether. (Fig. 1.)
Shell greatly elongated or lengthened posteally, the anteal or
PURBECK BEDS OF THE VALE OF WARDOUR. 247
anterior side rounded and somewhat steep; the base (inferior or
ventral border) flattened; the postero-dorsal (umbonal or superior)
-border concave and much elongated.
Fig. 1.—TZriyonia densinoda, Ether.
Umbones pointed, small, but prominent or elevated and slightly
recurved, antero-mesial, or placed within the anterior third of the
valves.
Area moderately wide, flattened and filled with reticulated costelle,
which are minutely and delicately nodulated or tuberculated ; it is
bounded by two carine, the outer densely or closely nodulated, in-
creasing in width from the umbo to near the extremity of the pos-
teal side, then merging into the system of tuberculated transverse
costee ; or the extreme posteal border possesses many irregular lines
of growth due to the elongation of the tubercles. ‘The inner
carina, or that bordering the escutcheon, consists of a series of minute
tubercles which are immediately surmounted by the tranverse wavy
ridges of the escutcheon. The median sulcus, or mesial furrow,
is well defined. The escutcheon is remarkably large, having trans-
verse Wavy rugee resembling those occurring in the Neocomian Qua-
drate. The shell (valve) possesses regularly and concentrically
arranged tuberculated or knotted rows of coste; about 40 range
from the umbo to the posteal attenuated border. Those tubercles
upon the posterior third of the valve, below the area become elongated
and less regularly arranged than those of the umbonal region, where
they are closely concentrically arranged.
Affinities and Differences. —In outward ornamentation 7’. densinoda
s 2
248 EK. ETHERIDGE ON A TRIGONIA FROM THE
mihi, much resembles 7’. tenwitexta from the Portland Oolite of
Portland, Devizes, Crookwood and Tisbury; but the shell is more
depressed and lengthened posteriorly than 7’. tenwtexta, and does
not possess the antecarinal sulcus or space of that species, which
occurs in all the known Jurassic Glabrae, and which is so essentially
characteristic of the Portland group.
The ornamentation is that of the Upper-Jurassic Glabree ; but the
escutcheon, which is remarkably large and possesses transverse
ruge, agrees with that of the Neocomian Quadratz, to which it
allies the species.
All the Neocomian Quadratze have the escutcheon ornamented,
and therefore distinct from that part of the tuberculated Jurassic
species in which itis plain or unornamented. Again, the Cretaceous
Scabree have also ornamented escutcheons; but the latter are alto-
gether different and far removed from the Jurassic Trigome.
I therefore regard this new species of Trzgonia as atransition form,
tending to connect the Portlandian Glabre, through its ornamenta-
tion, with the Neocomian Quadrate, through the ornamented and
peculiar or characteristic escutcheon. Its stratigraphical position
at the highest portion of the Jurassic system indicates a zoological
change in progress as regards the genus Zrigonia, constituting an
important feature in the history of the genus, no other example of
which, so far as I am aware, is known in rocks representing the
Purbeck formation, either British or continental.
This new species falls under the group or section Glabre, founded
by Agassiz upon very insufficient “data, and described by him as
beivg without ornamentation, having no tubercles or costa. The
shells of this group are usually ‘“inflated-ovate or ovately-oblong ;
and the area is only slightly separated” from the rest of the valve.
Mesially, or anterior to the position of the marginal carina, there is
a smooth space which commences at the apex (umbo) or near it, and
gradually widens downwards to the posteal border. This smooth
space is more depressed than any other portion of the valves, and is
distinctly impressed by lines of growth.
In this group the “ anteal ” portion of the valves possesses costee
more or less prominent, usually small, closely arranged, and either
plain or tuberculated. The number of species belonging to this sec-
tion is seven, six of which are Jurassic, the remaining form being
Cretaceous (2. excentrica, Park.).
Our species is closely allied to those forms known in the Portland
rocks under the name 7’. gibbosa, Sow., 7’. Damonana, de Lor., 7’.
Manselli, Lycett, and 7’. tenwitexta, Lycett, and. especially to the
last named, from which, however, it differs in form and characters.
Nore on the Strata. By the Rev. W. R. Anprews, M.A.
Mr. Andrews has drawn up the following description of the
Purbeck beds of the Vale of Wardour ; and any of the sections would
suffice to read aright the succession and position of the fossil under
consideration.
PURBECK BEDS OF THE VALE OF WARDOUR. QAO
Mr. Andrews says, “the Purbeck strata occupy an area of from
five to six miles square at Teffont Ewias, Chicksgrove, Lady Down,
&c. in the centre of the Vale of Wardour, and rest conformably
upon the Portland group, sometimes, but not always, separated by a
thin band of dark clay. These estuarine deposits have been consi-
dered to belong to the Jurassic system, in consequence of their pre-
senting remains of animal life nearer in affinity with the Jurassic
period than with the Wealden above, and also from the fact that the
marine Portland beds pass into the freshwater Purbecks without un-
conformity, and generally with an ancient land surface at or near the
junction ; the same area too (for the Portland beds are always capped
by the Purbecks) which formed the bottom of the Portland sea, became
when raised, first the support of the ancient forest, and then, when
again slightly depressed, the delta of some great river, and this
without any unconformity or denudation, which would imply a great
lapse of time.
“<The Purbeck beds in the Vale of Wardour are comparatively much
thinner than those exposed on the Dorsetshire coast, and here pre-
sent only about 60 or 70 feet, belonging entirely to the lower and
middle divisions.
“‘ Whether the Upper Purbecks were ever deposited here, it is im-
possible to say. These Purbeck beds thin out rapidly on the coast,
passing from K. to W., or from Durlston Bay to Portland Bill, and
also from 8. to N., passing from the same exposure at Swanage
through the Vale of Wardour to the thin capping at Swindon.
This thinning-out may have been due to the north and west sides
of the estuary being raised and above water when the Upper Purbecks
were being deposited in the south and east—a supposition which
is borne out by the Purbeck at Swindon, shown by Mr. Blake to
be ‘in point of time as old as some parts of the Portland.’ Or,
on the other hand, the upper beds may have been deposited and
denuded—a supposition not improbable when we remember that
the Cretaceous system rests quite unconformably on these freshwater
beds, e.g. the Gault in the Vale of Wardour overlapping the beds
below.
*« New quarries, opened since Fitton wrote his memorable paper,
have supplied some very interesting fossils, amongst which is the
new Trigonia (T. densinoda).
“ At the junction of the Purbeck beds with the Portland strata
there generally occurs a thin bed of dark clay; and some few feet
above may be seen an ancient earth or land surface, which is, in
places, as much as 2 feet thick. This bed has in it large pieces of
coniferous wood and a Cycad, as in the Isles of Portland and Pur-
beck. The “cap” as it called, is here visible, and has yielded
some interesting Mollusca, besides several species of fishes, and
a very much larger form of Archeoniscus than A. Brodie. The
beds immediately above the Middle Purbecks are not well exposed,
they consist (as on the coast) of soft shales with Cyprids and marls,
affording no good stone worth the quarryman’s labour. These,
I presume, would be equivalent to the soft cockle-beds of the
Durlston section.
250 REV. W. R. ANDREWS ON THE
“‘ At the top of the Lower Purbecks and in the Middle Purbecks
much useful stone occurs, and has been extensively quarried both
for building-purposes and for burning into superior lime; from these
exposures some interesting fossils have been obtained.
‘Thick beds of a hard grey marl at the top of the Purbecks, very
similar in appearance to the insect-beds of Durlston, but containing
Cyprides, here afforded some few insect-remains, several species (6)
of fishes, and Archwoniscus (the fishes are the following—
Microdon radiatus, Ophiopsis breviceps) ;
Plewropholis,
also Turtle and Crocodile remains. The insect-remains are not so
plentiful as at Durlston, a comparative scarcity arising from the
terrestrial condition of these beds in the Vale of Wardour, as evi-
denced by the presence of Cyprides.
‘“‘ Passing up through the ‘‘ cherty freshwater ” beds, which here
contain, as in Dorsetshire, Paludine and Cyclades beautifully imbed-
ded in flint, we arrive at one of the most interesting beds of the whole
series, a marine bed called, in the island, the “Cinder.” Although
it is much reduced in thickness from 12 ft., crowded with Ostrea
distorta, still, in the Vale of Wardour, it maintains its marine cha-
racter, and, as elsewhere, from its hard enduring nature, has outlasted
many softer beds. Beside the Ostrea distorta which is scattered
through it, two species of Zragonia occur, 7’. gibbosa and a new
species which Mr. Etheridge has named 7’. denstnoda, which has not
occurred in any other formation and, according to Mr. Etheridge, is
of much paleontological interest, arising from the fact that it has
characters connecting it with the Jurassic Zrigonia-group Glabre,
on the one hand, and Cretaceous forms of the group Quadrate, on
the other. Occurring, as it does, in beds of a transitional character
between the Jurassic and Cretaceous, it is more interesting still.
‘‘ Higher up in the Middle Purbecks occurs an extraordinary abun-
dance of the fossil Isopod Archconiscus Brodiei, sometimes so closely
lying together that 250 specimens haye been obtained on a slab not
larger than one foot square. The 8 or 10 feet of red and yellow
stratified sandy clays which are here found on the top of the Pur-
becks, are possibly the Wealden. They rest upon an eroded surface
of limestone, but otherwise present no unconformity. It is remarkable
that these Wealden beds so often cap the Purbeck series, a fact
that seems to indicate that the same area which served for the delta of
the Purbecks performed the same office for the Hastings series, with,
however, this difference—that the source from which the materials
came must have been different, although the ancient river may
have served for both formations.
“« Endogenites erosa, not hitherto clearly proved to belong to any
other horizon than the Wealden, has been found in these red and
yellow sandy clays in situ ; a stratified bed above contains a small
Modiola and Cyrena; but whether Wealden or Purbeck, I am not
able to say. Hndogenites erosa occurs in a similar section half a
mile to the east.”
PURBECK BEDS OF THE VALE OF WARDOUR. 251
The Rev. Mr. Andrews has made a careful section of the railway-
cutting at Teffont, which shows the Hastings beds and the Middle
and Lower Purbecks. The Rey. O. Fisher marked the divisions on
the section. Mr. Andrews is of opinion that no higher Purbeck
beds occur in his neighbourhood than those shown on the section,
and that the Hastings series were deposited upon the eroded Purbeck
strata; the Purbeck strata continue 50 ft. or more below the base
of the railway-cutting, as there are many quarries in the neigh-
bourhood with many feet of Purbecks resting upon the Portland
beds. The section in the railway-cutting ends 7 ft. below the
“cinder bed;” but the quarry near the Rectory has been carried
19 ft. below the ‘‘ cinder,” into hard grey marls, which are burnt
for lime, and contain many fish, insects, Archwonscus, Cyclades,
Cyprides, &c.
The following 1s a detailed section of the Portland beds in the
railway-cutting, drawn up by Mr. Andrews, which, although similar
to the woodcut-section on p. 252, nevertheless enters more into the
particulars of the beds, both as to thickness and succession, and will
doubtless be found useful if the district is visited and examined : —
No. ft. in. Surface.
Rif 1. 2 Q Brown earth, with scattered flints, passing into
S| 2. 2 Q Redand yellow sand, with a few scattered flints.
3 | 3. 1 6 Grey sand with red streaks, passing into
=e | 4. 1 O Grey sandy clay, red and yellow layers.
a { 5. QO 2 Purplish red clay, laminated.
5 6. 0 6 Green clay, light-red lines.
= | Te 4 Layer of iron in lamine.
\ 8. 1 Green clay, red irony lines of variable thickness, resting
unconformably on the bed below, and running down
amongst the lumps.
( 9. 1 90 Worn flint-shaped lumps of hard marl, vertical fracture.
10. 1 6 Sandy, with perished shells in layers.
| 11. O 6 Clay, red and grey, in lamine.
12. 0 2 Very red sandy rock, sometimes blue and grey, with large
bivalves, Ostree.
| 13. 1 0 Limestone layers in sandy clay.
14. 0 9 Thin laminated brown sandy limestone.
@ 15. 1 0 Hard sandy stone, often red outside, ripple-marks on
® the top.
= 16. 1 0 Composed of perished shells, thin layers of limestone
as and a line of ‘“‘ beef” about the middle.
. | 17. 1 4 Redand yellow sand in layers. Ostree.
eS Ss. Clay, thin-laminated, soft and yellow; impressions of
2 Archeoniscus.
2 19. 0 9 MHard blue and brown marl, Archeoniscus, Cyprides,
Ay 4 Cyclas, Ostree, insects’ wings.
x 20. 0 3 Laminated thin white limestone and sand.
oS 21. 0 3 Hard red sand rock, occasional streaks of blue; oysters
= and impressions of large bivalves.
22. 0 2 Soft sandy limestone.
Carried a
forward }16 13 Le de
Fig. 2.—Section of Purbeck-Beds in a Railway-cutting 11 mile west
of Dinton ae Vale leh Wardour, (Scale, 1 inch ‘to 1 foot.)
MIDDLE
PURBECKS.
LOWER
PURBECKS.
—
i
Me pal toon
VILLE
re
Surface.
Flints, “ trail.”
Yellow and red sandy clays. Endogenites erosa.
Hard marl, eroded surface.
Sandy, perished shell in layers.
Laminated clay.
Red sandy rock. Ostrea.
Limestone, laminated.
Red and yellow sand. Ostrea.
Archeoniscus, Cyprides, Cyclas, Ostrea.
Hard blue marl. Archeoniscus, Insects.
Hard red sandy rock. Ostrea.
White fissile limestone. -Archeoniscus.
Brown limestone rock. Ostree and Fish.
« Beef.”
Chert.
Cinder-bed. Ostrea distorta and Trigone
(Lf. gibbosa and T. densinoda).
Hard limestone.
Sandy rock.
Old earth-surface.
“TLias.” Cyprides, Archeoniscus, Fish.
Clay.
Hard crystalline rock.
ON THE PURBECK BEDS OF THE VALE OF WARDOUR. 953
a
Lower Purbecks.
ING, Vy Teng
Brought ‘
orward i 16 1a
= 23. 1 4 Soft white limestone, laminated, ‘‘ White bed.” <Archeo-
S NUSCUS.
S 24. 1 0 Brown rock, shelly, large bivalves, oysters, fish-remains.
iS | 25. Oolitic stone, brown.
Ss | 20. Soft limestone, vertical fracture.
2 s Pipe Oa os Beet.
24 28. 0 6 Sand and limestone in layers.
2 | & 29. 0 2 Chert.
& | = 30. 0 2 Sandy clay, dark brown, shelly.
© | w ol. 2 5 Hard grey marl, and brown soft rock, very varying in
nS, 3 their proportions, sometimes the hard marl taking up
= in all the space, and vice versd. ‘‘Cinder” containing
5 scattered Ostrea distorta, and T'rigonie.
6 32. 3 0 Hard crystalline limestone, in 1, 2, or 3 layers, with thin
sand or clay between, blue outside, and containing
lumps of chert, Cyclades in clay parting with vegetable
| remains and Paludine. Cyclades and Ostree in the
| chert.
\ 03. 1 0 Sandy rock, yellow.
(
| 34. 0 2 Dark clay.
4 39. 1 6 Hard grey marl. Insect-beds of Purbeck.
36. 0 2 Clay.
| of. Hard crystalline rock, shelly.
c
23 65
Discussion.
Mr. Hutxs remarked that the fauna of the “ Cinder-bed” being
very limited, even where it was best known, namely at Swanage,
any addition to it was of great importance. The discovery of the
species described by Mr. Etheridge was especially important, the
fossil being so strongly characterized that no doubt could be enter-
tained as to its distinctness, while, at the same time, it was par-
ticularly interesting as binding together two other forms, an older
and a younger one, and thus, to a certain extent, bridging over the
gap between the Jurassic and Cretaceous Trigonie.
Dr. Duncan thought that the Wealden-Purbeck forms a series
intermediate between the Cretaceous and the Jurassic.
Prof. Srrtny agreed with the author that the form is a new
species.
The Aurnor stated that he had shown the specimen to Dr. Lycett, .
who agreed with him as to its peculiarities of character.
254 W. J. SOLLAS ON A NEW LYSSAKINE HEXACTINELLID
18. On Astroconta GRANTI, a new LyssakINE HExACTINELLID from
the SILURIAN Formation of Canapa. By W. J. Sottas, Esq., M.A.,
F.R.S.E., F.G.8., Professor of Geology in University College,
Bristol. (Read February 23, 1881.)
By the great kindness of Lieut.-Col. Charles Coote Grant, I have re-
ceived a valuable collection of fossil specimens from the Silurian strata
of Hamilton, Ontario. J hope, as opportunity serves, to offer de-
scriptions of the more interesting of these fossils, and in the following
short paper make a beginning by describing an incompletely silici-
fied specimen of chert, which by its remarkable similarity to the chalk-
flints of Trimmingham arrested my attention when studying those
bodies. The specimen in question is a small piece (1 inch cube) of
greyish siliceous dolomite with a gritty granular texture; on one
face it bears a carbonized Hydrozoon, on another a silicified Polyzoon,
and on a third shows the opening of a long winding cavity which
extends into the interior. From the sides of this cavity some long
cylindrical rods, very suggestive of sponge-spicules, were seen
conspicuously projecting: ‘under the microscope by reflected light
they were seen to be covered with an irregular crystalline deposit,
which made the resemblance to spicules less striking than when exa-
mined by the unassisted eye. The specimen was now broken into two
pieces, and the part containing the rods and cavity placed in dilute
hydrochloric acid. Solution with faint effervescence took place; and
after standing for twenty-four hours the supernatant liquor was
poured off for subsquent examination, while the sediment and
small piece of siliceous dolomite remaining were well washed and
further examined. From the sides of the cavity in the dolomitic
chert, cylindrical rods were still seen projecting, and under the
microscope were found to have lost their irregular outline and
at the same time to have somewhat diminished in thickness ;
evidently a crystalline coating had been dissolved away from them ;
and in the slender siliceous rods which remained one recognized at
once true sponge-spicules.
The sediment was next examined. It contained a number a large
siliceous spicules, some of which are figured on page 255, also some
small colourless transparent hexagonal prisms capped with six-sided
pyramids at each end, evidently quartz crystals, and, finally, some
minute rhombohedra, which were subsequently found to be mag-
nesite.
The Sponge-Spicules.—By reflected light the spicules appear snow-
white, with a vitreous lustre; by transmitted light they are glassy and
translucent ; when immersed in water, glycerine-jelly, or Canada-
balsam, they become quite transparent, except in places where they
are traversed by a minute black spongy network which appears
white and shining with reflected light, and evidently contains air:
when this is displaced by the liquid medium, the spicule becomes
FROM THE SILURIAN FORMATION OF CANADA, 255
Figs. 1-11.—Spicules of Astroconia Granti, Sollas. (All magnified
40 diameters, except figs. 38, 5, and 7, which are magnified 104
diameters. )
256 W. J. SOLLAS ON A NEW LYSSAKINE HEXACTINELLID
transparent throughout; it is frequently colourless, but sometimes
presents a faint yellowish brown tint either in places or throughout.
The surface of the spicule has a rough irregular appearance when
examined dry, which disappears, however, on immersion in balsam,
being evidently due to a crystalline incrustation (magnesite). When
this is removed the sides of the spicules appear as neat continuous
lines; the axial canal is also quite sharply defined, and is sometimes
not more enlarged than in recent deciduous spicules, though
occasionally it is so wide as to reduce the spicule toa mere shell. In
some instances it has been infilled with silica, so as to appear as a
cylindrical rod projecting from what remains of the spicule in which
it was formed (fig. 8, p. 255).
The spicules are not excavated by rhombohedral pits like those
seen in Hyalostelia Smithi, Young, from the Carboniferous Limestone
of Scotland ; but sometimes they are pitted all over with hemispherical
cavities such as are seen in deciduous and fossil spicules, and which
can be produced artificially in recent spicules by solvent agents.
With polarized light all the spicules give brilliant colours, and
much more vividly than those from the chalk of Trimmingham ; the
colours frequently occur in spherical patches, as though crystallization
had been set up about various centres within the spicular substance ;
one might term it an internal botryoidal structure, though the
spicules are never botryoidal externally ; somtimes the polarization-
effects show clearly that the spicule is composed of minute prisms
radiating outwards from the sides of the axial canal.
In concluding this brief account of the mineral state of the spicules,
I may remark that, though highly crystalline, they are almost if not
quite as well preserved as those of Hyalostelia from the Carboniferous
formation ; and this is certainly surprising when we consider their
ereater age and much smaller size. The conditions under which the two
sets of spicules were preserved were evidently very different, however ;
for Hyalostelia does not appear to occur in association with deposits of
chert as is the case with Astroconia. Hyalostelia is possibly preserved
to us chiefly by reason of the magnitude of its spicules, Astrocoma
chiefly by secondary silicification.
We now pass on to a description of the forms of the several spicules,
which are figured on page 255, all being magnified 40 diameters
except figs. 3, 5, and 7, which are magnified 104 times.
Fig. 1 is the commonest form, occurring in fragments of various
lengths, that represented being the longest seen. It is almost exactly
cylindrical; and the axial canal maintains a straight course and even
width throughout. Its natural termination has not been seen; but
probably it was pointed at both ends, and formed the acerate
spicule of the sponge.
Fig. 2 looks at first sight like the trifid spicule of a Tetractinellid ;
but careful examination shows the presence of four rays, of which
that marked a is one; though as here represented it appears
merely as a bifurcation of the one in front of it. By examining the
other side of the glass slide on which.the spicule is mounted its real
nature is readily made out; moreover I was able to turn an almost
FROM THE SILURIAN FORMATION OF CANADA, 957
exactly similar spicule over on its head, so that its shaft projected
vertically ; the four capitular rays could then all be seen in one view.
The axial canal of the shaft is prolonged upwards past the common
origin in the head, and, no doubt, once extended into a short vertical
spicule ; indeed the companion spicule showsas much. In addition
to this axial spine, containing a continuation of the canal, the head
is ornamented by conical tubercles given off in the same direction
from the upper surface of the capitular rays (as shown in the figure).
I take this spicule to have projected radially from the surface of
the sponge-body, the shaft being directed inwards and the capitular
rays expanding parallel to the surface of the body, as in the similar
spicules of Holtenia and Rossella; it has not the appearance of an
anchoring spicule.
Figs.3 and 3a. These two drawings represent the same specimen,
the upper one taken before immersion in a liquid medium and by re-
flected light, the lower one by transmitted light when mounted in
Canada balsam. They are magnified 104 diameters: so that, if
represented on the same scale as the other figures, they would not be
quite so large as the spicule represented in fig. 6. he noticeable
feature is the presence of spines on the rays, directed in all cases
towards the ends. ‘The rays were evidently at least five in number ;
probably there were six. |
Fig. 4. The four rays of this spicule are directed downwards
below the plane of the paper ; near their origin they each give rise
to a large bifid spine inclined upwards away from the plane of the
paper. It is probable that this specimen once formed the head of a
spicule like fig. 2.
' Fig. 5. This spicule (X 104) is chiefly remarkable for its spinose
rays: on the longest but still broken ray three spines are given off
from one side, and a fourth, represented in plan by a circle, from
the adjacent side at right angles.
Fig. 6. The proximal half of the rays is thicker than the distal
end, which is long, slender, and directed downwards, the proximal
half lying in the plane of the paper. The thicker part of the rays is
spined—the spines (so far as one can judge from the three which
remain on one of the rays) being arranged spirally, and two of
them arising near the origin of the slender extremity.
Fig. 7. This represents a fragment of a cylindrical spicule magni-
fied 104 diameters, with the axial canal filled up with silica, which
now projects at both ends like an acerate spicule run through the
middle.
. Fig. 8 is also a fragment of a cylindrical spicule; it shows the
hemispherical pits which have been eaten out of its surface.
Fig. 9. This is one of the most frequently occurring forms ; it is a
large simple sexradiate—the rays having a cylindrical form, only
slightly tapering towards their broken extremities. The axial
canals are regular and clearly defined. ‘This is probably one of the
staple body-spicules of the sponge.
Fig. 10 is a smaller spicule of the same kind.
Fig. 11. This is less like a Hexactinellid spicule than the others,
258 W. J. SOLLAS ON A NEW LYSSAKINE HEXACTINELLID
possibly owing to its being incomplete and yet simulating complete-
ness through a sharpening of its ends by solution. The axial canal
can be clearly traced through one half of it only, the other half being
rendered opaque by the close firm network of cavities which exca-
vate it.
Leaving out of consideration the last, which is a doubtful form,
and a few other fragments not figured and quite undeterminable, one
may safely say that all the spicules extracted from the small
fragment of dolomitic chert are distinctly Hexactinellid; and it
would appear that we probably have here, not a heterogeneous mix-
ture of spicules derived from several kinds of sponge, as is usually the
case in chalk-flints, but the much rarer case of a natural assem-
blage of forms derived from a single individual. For this group of
forms we propose a distinct name, Astrocona Granti, the specific
designation being given in honour of the indefatigable observer to
whom. we are indebted for our knowledge of the sponge.
The Quartz Crystals—These do not differ in character from those
described from the Carboniferous Limestone by Mr. Wardle and in
my papers on Catagma (Ann. & Mag. Nat. Hist. ser. 5, vol. u. p. 361,
fig. 3), and on Flints (vol. vi. p. 445). I have also called attention to
the important part which such such crystals play in rock-formation
by pointing out that certain beds of sandstone in the Eden valley
appear to partly consist of them. If we knew the bulk of these beds,
we might calculate the amount of limestone which must have been
denuded to produce them, on the assumption that this limestone con-
tained 1 oz. of crystals in every 10 lb. of rock, as is the case with
that at Buxton at the present day. I believe that in these quartz
crystals, derived undoubtedly from siliceous organisms, we have also
the key to the origin of the “krystallinische Quarzpsammite” of
Naumann, which occur in several formations on the continent (Zir-
kel, Lehrbuch der Petrologie, vol. 11. p. 575). They are nothing
but the insoluble residues of limestone masses which have been
dissolved away by the action of subaerial waters*. If this be so,
we have in these crystalline sandstones the last stage of one of those
beautiful cycles or, rather, spirals which appear to characterize the
operations of nature : the silica derived from the disintegration of igne-
ous rocks is carried in solution into the ocean and there built up by
living organisms into forms of endless diversity and exquisite beauty ;
this organic silica again yields to solvent influences and afterwards
crystallizes out amidst calcareous sediments in perfectly formed —
crystals of mineral quartz; the calcareous rocks elevated above the
sea-level are exposed to water and the weather; solution proceeds
apace; and after the carbonate of lime has become dissolved away, the
* This statement is too absolute. The beautiful observations of Mr. J. A.
Phillips, F.G.S., in complete accordance with those of Prof. Bonney and
Dr. Sorby, show that crystalline quartz-sandstones are sometimes formed in a
quite different manner—indeed, that the formation of quartz crystals has been
subsequent to that of the sandstone as a whole. In deciding upon the origin of
such sandstones, we shall have probably to be guided by the circumstances in
each ease, before we can say certainly that the constituent quartz crystals are
original or superinduced formations.
pe
FROM THE SILURIAN FORMATION OF CANADA. 259
minute quartz crystals, uninjured and unworn, are washed into the
sea to constitute afresh the mineral sediments of the earth’s crust.
Rthombohedra of Magnesite.—These were left on the solution of
the limestones in dilute hydrochloric acid, the majority of them
occurring in a free and separate state, but a few imbedded in small
fragments of chert, just like those figured by Professor Renard in his
memoir on the ‘ Phthanites du Calcaire Carbonifere de Belgique’
(Bull. de PAcad. Roy. de Belgique, 2™° sér. t. xlvi. p. 471, 1878). To
determine their nature, as well as that of the rest of the limestone,
J made a preliminary qualitative analysis, first of the solution pro-
duced by the action of hydrochloric acid, and next of the undis-
solved residue. The former contained lime and magnesia, carbo-
nate of lime and phosphate of magnesia being precipitated in appa-
rently equal bulk ; the residue was boiled with strong hydrochloric
acid, and the resulting solution analyzed; it contained a little iron,
not a trace of lime, but a considerable quantity of magnesia; hence
one might conclude that that part of the rock which is not chert, is
dolomite, while its included rhombohedra, which were set free on
solution, are magnesite; and a quantitative analysis is scarcely
necessary. _
The Geological Horizon.—The rock specimen was obtained from
the chert beds of the Niagara Limestone, which is homotaxial with
our Wenlock Limestoue. It affords the oldest known instance of the
associated occurrence of siliceous sponge-remains and chert. On the
one side of a fragment of rock we find free spicules still siliceous,
together with quartz-crystals imbedded in dolomite—on the other a
mass of chert, in which spicules are rarely seen, and then usually as
hollow casts, but which contains remains once calcareous (such as
the Polyzoon before mentioned) now converted into silex.
Discussion.
The PresrpEnt said this was the oldest sponge next to Proto-
spongia. The author’s remarks on it were most valuable, and those
on the collateral subject very interesting. It was to be hoped that
Mr. Maw would discover in the English Wenlock Limestone some
similar microscopic forms.
Prof. Duncan said it was interesting to see the modern Hexacti-
nellids thus foreshadowed. Very lately he had seen one of the
spicular forms described by Prof. Sollas in a form he had just
described. He quite agreed with the author in assigning this form
to the Lyssakine Hexactinellids. There could be no question as to
the solution of the spicules in sea-water, as he had lately seen
evidence of it in specimens from deep-sea dredgings. The results of
Mr. Maw’s washing promised to be very interesting. He had
examined many, but had not yet found either sponge-spicules or
Foraminifera.
Prof. Rupert Jones remarked that there are different kinds of
“‘chert,” and expressed his opinion that Mr. Sollas had well
260 ON A NEW LYSSAKINE HEXACTINELLID FROM CANADA.
explained the origin and formation of the spicular strata which
he had described on this and other occasions. He thought that
Dr. Wallich’s hypothesis of the conversion of extensive layers of
sponge-protoplasm into black flint elucidated many, but not all, of
the phenomena connected with the origin of such siliceous strata as
flint and chert. He stated that sponge-spicules, and numerous
other Microzoa from the Upper Silurian shales of Shropshire, had
been noticed lately by Mr. Smith of Kilwinning.
Dr. Hicks said that it was remarkable that chert was not asso-
ciated with Protospongia, as, on either Dr. Wallich’s or Prof. Sollas’s
view, might have been expected.
Prof. Jupp said that, as the solution of siliceous organisms had
been recently doubted, Prof. Sollas’s observations were of additional
interest. He himself fully believed that this solution did take
place; now and then he had found, in examining the residues left
by dissolving chalk in acid, the thickest portions of siliceous spicules
still remaining not quite destroyed in chalk.
Prof. Sottas replied that he believed a spicule had been described
by Mr. Carter similar to that mentioned by Prof. Duncan. The one
described now by him, however, was much more robust. He had
never been able to find spicules in the Wenlock. He could not
comprehend what Dr. Wallich’s views really were. That none of
the fossil siliceous spicules which the author had described were
originally calcareous was quite certain. As for Protospongia, it
did not occur in hmestone, and bore a very small proportion to the
mass of the bed; and this might account for the absence of the
chert.
Quart. Journ.Geol.Soc Vol XXXVILPI IX.
WMintern Bros amp
IGS WELAINTOS
+
J
AVLUROSAU
PROF. OWEN ON THE ORDER THERIODONTIA. 261
19. On the Order TumrtopontiA, with a Description of a new Genus
and Species (ALUROSAURUS* FELINUS, Ow.). By Prof. Owen,
C.B., F.R.S., F.G.S. (Read March 9, 1881).
[Prats IX.]
Or Permian and Triassic Reptilia the most interesting, those that
help to fill the hiatus separating the mammalian Marsupials from
the cold-blooded Vertebrates, seem to me to be the extinct species
constituting, or referable to, the Order THERIoponmTrIA.
To the characters of this Order given in my ‘ Catalogue of the
Fossil Reptilia of South Africa’, viz. “‘ Dentition of the Carnivorous
type, incisors defined by position and divided from molars by a large
laniariform canine on each side of both upper and lower jaws,” may
now be added “dentition ‘monophyodont’” +. At least I have not
had evidence of an immature specimen showing a milk-series of
teeth to be succeeded by a permanent series; but if such should be
found in any of the extinct Reptiles of the present Order, such Order
will be “ Diphyodont,” like the Mammalian Carnivora; for there is
no evidence of any third set of teeth to follow those which may have
been preceded (though I doubt it) by a first or deciduous set. Of
the adult dentition, whether it be “ first ” or “ second,” the molars,
as a rule, are inferior in size to the incisors, as both are markedly
less than the canines. Add to these characters, “‘ humerus perifo-
rated by an entepicondylar foramen”$.
The Reptiles so distinguished or characterized are already refer-
able te several genera ; and although I fully recognize the artificial
character of a more or less forward extension of the ossified ‘‘ septum
narium,” there was a convenience in disparting the Theriodont
genera known in 1876 into “ Mononarialia” and “ Binarialia”||.
At that date the ‘‘ Mononarials” included Cynodraco 4], Cyno-
champsa**, Cynosuchus ++, Galesaurus tt, Nythosaurus §§, Scalopo-
saurus || ||, Procolophon 44 ; the “ Binarials” included Lycosaurus ***
and Tigrisuchus;ty. Gorgonopsttt manifested a third narial
modification.
To this series have since been added species referable to some of
the foregoing genera, and, also to a genus T%tanosuchus §$$. The
latter was founded on fragmentary fossils not yielding a narial cha-
* Gr. aidoupos, cat; catpos, lizard. t Ato, 1876, p. 15.
t Anatomy of Vertebrates, 8vo, 1866, vol. ii. p. 268.
§ Ib. p. 19, pl. xix. figs. 2&3 4,h; Quart. Journ. Geol Soc. August 1876,
p: 361, cut, fig. 2, h.
|| Catalogue, u¢ supra, pp. 15, 17. €| Ibid. p. 19.
** Quart. Journ. Geol. Soc. vol. xvi. 1860, p. 61, pl. iii.
tt Catalogue, ut supra, p. 21.
tt Quart. Journ. Geol. Soc. vol. xvi. 1860, p. 58, pl. ii.
§§ Catalogue, ut supra, p. 24. || || Ibid. p. 24. {4 Ibid. p. 25.
F~ Ubid. p: 15. ttt Ibid. p. 17. {tt Ibid. p. 27.
§§§ Quart. Journ. Geol. Soc. vol. xxxy. 1879, p. 189, pl. xi.
Q.93.G.8. No. 146. a
262 PROF. OWEN ON THE ORDER THERIODONTIA,
racter; and with Tvtanosuchus, for the same reason, may be cited
Kutorga’s Brithopus and Orthopus, from Russian Permian, V. Meyer’s
Urosawrus, Fischer’s Rhopalodon, Hichwald’s Deuterosaurus, and
Twelvetrees’s Cliorhizodon, from the same zone and locality ; to the
Theriodontia belongs also Bathygnathus from the Trias of ‘“ Prince
Edward’s Island,’ North America*.
To add to this series of Theriodont genera, and, seemingly, to the
“‘ Mononarial” section, I now submit to the Society evidence of
another genus, dlurosaurus, exemplifying in a clear manner the
typical Theriodont characters, under modifications generically distinct
from those of the specimens above cited.
It is a skull, including both upper and lower jaws, with the orbits,
obtained by Mr. Thos. Bain from the Trias of Gough, in the Karoo
district of South Africa, and in the usual petrified condition of the
fossils of that formation and locality. The postorbital part of the
skull is broken away, and the border of the nostril has been slightly
fractured; but the rest of the specimen, with the dentition, is
instructively preserved.
The nostril (Pl. IX. figs. 1 & 2, 1) is terminal and vertical, and
shows no part of a septum; in shape it is a full transverse ellipse ;
what remains of the outlet yields in breadth 13 millim., in depth
9 millim. Lach orbit (ab. ib. 0) gives a full obliquely vertical
ellipse, 25 millim. by 20 millim. The facial part of the skull
extends two and a half times the fore-and-aft diameter of the orbit
in advance of that cavity. The hreadth of the upper jaw a little
behind the nostril is 26 millim., and gradually increases to 35
millim. near the orbits. The upper surface of the antorbital part
of the skull is moderately convex ; the sides are less convex, but not
flat; the vertical extent of the upper jaw at the middle of the molar
series is 34 millim., and decreases to 20 millim. above the incisors.
The skull has been subject to slight distortion ; but as this has
been effected without fracture, it may be concluded to have been
due to forces operating on the matrix after petrifaction, and when
the fossil was so encased as to be equally supported on every side
during the movements of the bed, such partial pressure haying
chiefly affected the left orbit (Gb. fig. 3,0) and a small part of the
same side of the skull in advance of it. From the degree in which
the sutures are obliterated, I conclude it to have come from a full-
grown and probably old individual, the state of the dentition sup-
porting that inference.
The premaxillo-maxillary alveolar border, as it recedes from
below the nostril, follows a slightly sinuous course, concave above
the incisors, convex above the canine and the molars; thence
straight to beneath the orbit.
The mandible is preserved, with the mouth close-shut; and the
mandibular teeth are hidden by the overlapping ones of the upper
jaw, requiring the sections made in two places for exposure. (ib.
fig. 3,c'). The symphysis mandibule (ab. fig. 3,s) is 27 millim. in
depth and 20 millim. in breadth where it is crossed by the upper
* Quart. Journ. Geol. Soc. vol. xxxil. p. 352, 1876.
AND ON ZLUROSAURUS FELINUS. 263
canines. From its fore border, formed by the incisive alveoli, it slopes
downward and backward, curving more directly backward where it
terminates below. All trace of a median symphysial suture is obli-
terated. The breadth of the mandible where the rami diverge from
the symphysis is 20 millim. The preserved length of the mandible
is 3 inches 3 lines; and this was probably that, or nearly that, of
the skull.
The suture between the maxillary (ib. fig. 1, 21) and malar (26) is
distinct, and shows the slender pointed hind end of the maxillary
terminating below the middle of the orbit, the lower or malar
boundary of which is here 8 millim. in depth.
Before the vertical parallel of the hind border of the orbit is
reached, the malar abruptly descends (ib. fig. 1, 26) at almost a right
angle to near the lower border of a deflected part of the mandible.
This descending part of the malar is broken off on the left side
Gb. fig. 3); and the mandibular depression which received it is there
exposed.
The mandibular ramus continued backward from the symphysis
is subcompressed, 12 millim. in depth beneath the middle of the
molar series, thence rapidly gaining depth, especially by a descent
and slight inflection of the lower border; the corresponding rise of
the coronoid plate is concealed by the malar. At the part where
the vertical extension of the mandibular ramus begins there is a low
tuberous outswelling of the external surface, behind which that
surface gradually sinks and describes a moderate concavity to the
angle of the jaw. |
A suture indicative of angular and surangular is not visible,
but that dividing such elements of the mandible from the dentary
one is manifest, as is also, along the lower narrow border
of the ramus (ib. fig. 3) the suture between the splenial and
dentary, showing the splenial to contribute to the hind part of the
large and strong symphysis (s) supporting the lower incisors and
canines.
The upper incisors (Pl. [X.figs. 1 & 3, 71-5) are ten in number,
five in each premaxillary, arranged in a semicircle or part of a
broad ellipse (fig. 3,2). The bases of the crowns are in contact,
save between the outermost and next tooth in advance.
There is but little difference in size; the first and last in each
premaxillary are the narrowest, the second and third the broadest ;
the exserted crown is best preserved in the fourth and fifth of the
right side (fig. 1), and in the fifth of the left side, the basal breadth
being 24 millim., the length about 10 millim.; they all appear
to have had the same simple laniariform character. When entire
they passed in front of and covered or concealed the crowns of the
lower incisors, the base of one of which is exposed behind the frac-
tured crown of its homotype above.
After an interval of 8 millim. extent the crown of the upper
canine (ib. c) extends downward, and with a feeble curve backward,
along a depression of like size and shape on the outer surface of the
mandible, which gains breadth for the socket of the lower canine
Tt 2
264 PROF. OWEN ON THE ORDER THERIODONTIA,
(fig. 2, c’) at the fore part of the depression for the reception of
the upper one.
The breadth of the base of the exserted crown of the upper canine
is 5 millim.; it rather suddenly narrows to the pointed end; the
length of the preserved exserted crown is 12 millim., a small part
of the apex being wanting. The crown is slightly compressed, with
a trenchant border on the hinder part which inclines somewhat
inward; there is an indication of a fine crenation of this border.
On the left side (Pl. IX. fig. 2) I had the outer alveolar wall of
the canine removed and exposed its root (c), extending upward and
slightly backward for twice the length of the exserted crown. The
root, as it rose, slightly expanded beyond the breadth of the crown,
and as gradually and slightly narrowed to the open end of the pulp-
cavity. There is not a trace of a successional canine; and the con-
dition of the pulp-cavity and petrified pulp, discoloured by the iron
of its blood, indicates renewal of the working part of the laniary by
continuous growth. In the course of this expository operation the
exserted crown of the mandibular canine (ib. c’) was exposed, 12
millim. in length, nearly that of the corresponding part of the maxil-
lary canine, in front of which it extends, but along the inner or median
level, so as to have been wholly concealed (as shown on the right
side, fig. 1) by the alveolar plate continued from the upper canine -
to the upper and outer incisor. There are few instances of carni-
vorous air-breathers in which the mandibular teeth are so completely
covered and hidden by the upper jaw, when the mouth is closed, as
in this and other Theriodont Reptiles.
After an interval about equal to that between the upper canine
and outer incisor, the molar series (ib. figs. 1 & 2, m) commences,
behind the canine. Of this series the crowns of five are exposed on
each side of the upper jaw; they are all of the simple, slender,
laniary type; the four anterior ones are divided by intervals of
about the basal breadth of those teeth, which is 14 millim. in the
first and second molars, and diminishes to 1 millim. in the fifth;
the crown, inclining a little backward in the three hindmost, gra-
dually narrows in each molar to a sharp point; the alveolar extent
of the five molars is 7 millim.
The toothless extent of the maxillary to beneath the fore border
of the orbit is 13 milim. The upper dentigerous tract in a straight
line from the foremost incisor to the hindmost molar is 45 millim.
On a cursory comparison of the Theriodont genera and species
now made known we discern a considerable range of variety in both
size and shape.
The extremes of size are exemplified by T%tanosuchus ferox * and
Scaloposaurus constrictus tT ; those of shape by the flattened head of
Galesaurus t and the compressed head of #lurosaurus (Pl. IX.).
The skull of Procolophon § is broad in proportion to its length ; that
* Quart. Journ. Geol. Soc. vol. xxxv. (1879), p. 189, pl. xi.
Tt Catalogue, wt supra, p. 24, pl. xvi. figs. 10-15.
t Quart. Journ. Geol. Soc. vol. xvi. p. 58, pl. ii.
§ Catalogue, wt supra, p. 25, pl. xx. figs. 4-7.
AND ON XLUROSAURUS FELINUS. 265
of Gorgonops* is narrow; but the ordinal characters are manifest
in all; only in the dwarfer and weaker species the relative size of the
canines decreases, as is the case with similar carnivorous Mammals.
Galesaurus planiceps and Aflurosaurus felinus form an equal-sized
pair of these ancient Triassic precursors of our existing cats, or rather
cat-like Marsupials. Galesaurus had 4—4 upper incisors like Dasy-
urus; Ailurosaurus had 5— > upper incisors like Didelphys; but the
molars of the foregoing and other Theriodonts indicate the lower or
earlier type that bore them in their simple acuminate form as in the
antecedent teeth; they had not advanced to the more complex modi-
fied character shown in the molars of the most carnivorous of either
12—12
marsupial or placental Fere. Galeswurus had as many as ;—, of
such molars ; in “lurosawrus they did not exceed, or at most by
one, the = manifest in the fossil here described.
Galesaurus, in the subject of the paper in the 16th volume of
our ‘ Quarterly Journal,’ still has the advantage over all the subse-
quently discovered Theriodonts in the entireness of the skull, espe-
cially in the occipital region; and we may infer, analogically, a
repetition of the reptilian characters of the cranium, indicative of
low cerebral development, in its coordinates.
If we next compare lurosaurus with the skull of Lycosawrus
curvimola ~, which, at the date of its extrication, was the next in
completeness to that of Galesaurus, we find the nearer affinity to
Ailurosaurus in the small number of molars, in the general propor-
tions of the skull, and in the extent and slope of the symphysis
mandibule ; but the incisor-formula is Dasyurine, and the facial
part of the septum narium is prominently manifested. But, of all
the previously described genera of Theriodontia I deem Lycosaurus
to have had the nearest kinship to Zlurosaurus.
I am indebted to Sir Bartle Frere, K.C.B., for kindly taking
charge of, and placing in my hands, the unique subject of the
present paper £.
EXPLANATION OF PLATE IX.
Ltlurosaurus felinus,
(All the figures are of the natural size.)
Fig. 1. Right side view of the skull.
2. Left side view of the skull.
3. Under view of the skull.
* Catalogue,ut supra, p. 27, pl. xxi. if Dbids pf pe 8:
{ For the discussion on this paper, see p. 270.
266 PROF. OWEN ON THE SKELETON OF
20. Description of Parts of the SkeLEron of an Anomopont REPTILE
(PLATYPODOSAURUS ROBUSTUS, Owen). Part. II. The Penvis. By
Prof. Owsn, C.B., F.G.8., &e. (Read March 9, 1881.)
[Puate X.]
Tue pelvis of Platypodosaurus, which has been relieved from the
matrix since the communication of the former paper*, includes. five
sacral vertebre (Pl. X. fig. 1, 1-5), the right ‘* os innominatum,”
62-64, and a large proportion of the iliac constituent of that of the
left side. Of the first, or foremost, sacral vertebra, s', the part of
the centrum in advance of the transverse processes, d!, is broken
away, but so as to show the apex of the anterior conical articular
cavity. The lumbar vertebra, which was articulated therewith, but
had become dislocated therefrom, is preserved in the contiguous
matrix ; and the shape and depth of the articular cavity of its centrum
are exposed (Pl. X. fig. 5).
The transverse process of the first sacral, d1, including both di- and
pleurapophysial elements, is short and massive: measuring one inch
and a half in antero-posterior diameter at its middle and narrowest
part, it rapidly expands to its articulation (and what appears to be its
confluence) with the ilium, 62. Behind the transverse process the cen-
trum is moderately constricted, but expands to form the joint with
the second sacral, of which joint the transverse diameter is 2 inehes.
The breadth of the entire vertebra is 44 inches.
The centrum of this second sacral vertebra (s 2) shows a greater de-
eree of constriction and a narrower inferior or ventral surface. The
transverse process (ib. fig. 1, d 2) extends from the anterior two thirds
of the upper part of the side of the centrum, is narrower than that
of the first sacral, but is longer, curving outward, and backward, ex-
panded at both ends, but most so where it abuts against the ilium.
The breadth of the second sacral is 5inches. The line of confluence
with and abutment against the ilium is better marked than in the
preceding vertebra.
The centrums of the third and fourth sacrals are less expanded
at their mutual junction than are those of the first and second
vertebrae. The transverse processes are rather shorter, as in that
of the third sacral, and this is narrower than those of the second
and fourth vertebre ; that of the fifth sacral is the narrowest.
Each transverse process of the sacrum expands at its outer end
so as to touch the contiguous one where it joins or coalesces with
the ilium. The foramina or vacuities so circumscribed decrease in
size from the foremost to the third pair, and change the oblong for
the subcircular figure. The hinder articular end of the fifth sacral
centrum, s5, is broken away, but in a minor degree than the fore
* Quart. Journ. Geol. Soc. for August 1880, vol. xxxvi. p. 414, plates xvi. &
XV.
Quart Journ Geol. Soc Vol XXXVIL PL %
Mintern Bros imp.
pLATYPODs \SAURUS ROBUSTU
A g
AS Foord delethth
AN ANOMODONT REPTILE. 267
part of the first vertebra; and a larger proportion of the arti-
cular concavity 1s there preserved. The entire breadth of this ver-
tebra is 44 inches.
Turning to the dorsal aspect of the sacrum (PI. X. fig. 3), the
hinder end of a lofty but narrow crest of bone, ns, due to confluence
apparently of the neural spines of the fourth and fifth sacrals, has
been worked out. The entire breadth of the fifth sacral vertebra is
5 inches. The condition of the spines of the antecedent sacrums
could not be determined. In the portion of a Dicynodont sacrum
described in the ‘ Transactions of the Geological Society,’ 2nd series,
vol. vii. pl. xxxiii. figs. 4 & 5, the short and thick spines of the
first and second sacrals are distinct, not confluent.
The section of the circular area of the neural canal of the fifth
sacral of Platypodosaurus gives a diameter of 6 lines; that of the
first sacral has a diameter of 9 lines; that of the last lumbar ver-
tebra one of 8 lines. ‘Thus we have an indication of an expansion
in the sacral region for the lodgment of the part of the myelon
transmitting the nerves to the pelvic extremities, which accords with |
the development of the limbs indicated by the femur of Platypodo-
saurus *, Comparing the sacrum above described with that of the
larger and more entire pelvis, the subject of a paper in the ‘ Geolo-
gical Transactions’ above quoted, I incline to regard “ five” as the
total number of the sacral or pelvic vertebree in Platypodosaurus *.
The degree of coalescence of these vertebre is such as to sustain
the anthropotomical ormammalian consideration of the coalesced mass
as one bone or “sacrum ;” but the ventral outlets are relatively
larger and the wings consequently less ossified. The general shape,
moreover, is quadrate rather than triangular, with deeper lateral
concavities between the subcarinate bodies and theiliac bones. The
present Reptilian sacrum consequently comes nearer in shape to that
of the Megatherioid mammals: but it includes fewer vertebral
constituents.
_ The length of such “sacrum” in Platypodosaurus is 74 inches ;
its breadth, greatest at the third vertebra, is 54 inches; it is con-
sequently more mammalian in character than is the sacrum of Dicy-
nodon =. In this larger example of the South-African reptilian pelvis
the sacral centrums are more constricted between the articular ends,
which are concomitantly more expanded. The space between these
sacral bodies and the ‘ossa innominata” is relatively greater; the
transverse processes are consequently longer, and retain more of the
ordinary reptilian rib-like character.
The ilac bone in Platypodosaurus rapidly expands from its attach-
ment to or confluence with the first sacral transverse process ; it ex-
tends and curves forward, outward and dorsad, with the convexity
mesiad, the concavity lateral. The extreme breadth is 43 inches;
and the anterior margin of the ilium runs almost parallel with the
* Loe. cit. p. 422, pl. xvii. figs. 6 & 7.
t Compare also with page 40, plate xxxvi. (pelvis of Dicynodon), in the
‘ Catalogue of Fossil Reptilia of South Africa, 4to, 1876.
{ Loe. cit.
268 PROF. OWEN ON THE SKELETON OF
portion of the long, slender, last lumbar rib (PI. X. fig. 5, pl) here
preserved. The outer border of the above expanse of the ilium is
produced into a narrow margin; but this subsides at the level of the
articulation with the second sacral vertebra, where the ventral border
of the ilium becomes thick, smooth, and convex. It thins off to the
dorsal border, which is here sharp; and the breadth of the ilium is
reduced to 24 inches. As the bone recedes it assumes a columnar
character, with an oval transverse section, gradually expanding,
where the right innominatum has been fractured, opposite its junc-
tion with the hinder sacrals, to a dorso-ventral diameter of 24 inches,
and a transverse one of 13 inch (ab. fig. 4).
The expansion of the bone after quitting the sacrum rapidly aug-
ments to the acetabulum (ib. fig. 2a), to which it contributes the
anterior and dorsal walls, the posterior and postero-ventral wall
(completing the circumference of the cup) being formed by the ischial,
63, and pubic, 64, constituents of the ‘os innominatum.” The
breadth of the iliac part of the acetabulum is 4 inches ; the diameter
of the outlet of the cavity is5 inches. There is a well-marked oblong
fossa, 14 inch in breadth, at the bottom of the cavity. The depth of
the cavity here is 13 inch ; and the wall is entire, and nearly an inch
in thickness.
The ischium, Y, contributes a rather larger share to the cavity
(GeIe Gailss 1 & 2, 63) than does the pubis..; Beyond the acetabulum
the pein contracts to a breadth of 2 inches 4 lines, where it may
contribute to the foramen (ib. fig. 20). This is subcireular and an
inch in diameter. Beyond the foramen the ischium loses. thickness
and gains breadth; but the confluence with the correspondingly
lamellate pubis is such as to leave no trace of their relative shares
in forming either the above foramen or the ventral wall of the pelvic
outlet. This wall, 6 inches in breadth, is strongly concave outwardly,
convex towards the pelvic cavity; both surfaces are smooth; and
the plate of bone so formed thins off to a symphysial border from
from three to four lines in thickness, and probably four inches in
extent.
The pubis (ib. figs. 1& 2, 64) gradually thins and auynik as it passes
from the acetabulum to the foramen, o. ‘The border forming the
subacetabular *‘ brim of the pelvis ” is from 7 to 8 lines in thickness ;
its border has been chipped; but, though not entire, it is free from
any indication of pectineal process, or of a prominence for the
support of a marsupial bone. The utmost care in exposing this
part of the pelvis failed to bring to light any such bones, or portions
of them. |
An accidental fracture, after exposition of the above-described part
of the pelvis, about 2 inches in advance of the acetabulum, gives the
transverse section (Pl. X. fig. 4) of that most contracted part of the
iliac constituent.
The dorso-ventral diameter of the anterior outlet of the pelvis is
8 inches; the extreme transverse diameter is 54 inches.
The place of the ischiadic notch, 2, which in most Bruta becomes
a foramen, is marked only by a feeble concavity of the postaceta-
an ae
a
AN ANOMODONT REPTILE. 269
bular border of the ischium : the “‘ tuberosity ” is indicated at ¢, fig. 2.
The extensive ischio-pubic symphysis (fig. 2, y,y) may have been
obliterated by continuous ossification, as in the pelvis of Dicynodon
above compared*, where it projects, ridge-like, between the broad,
outwardly concave, ischio-pubic plates. The parts of the dorsal
surface of the plates of Platypodosaurus exposed in the block of
tmatrix show the hinder half of a continuous crest of bone (1b. fig.3,7s),
due to confluence of the neural spines of the third, fourth, and fifth
sacrals. It may have been continued further forward.
The last lumbar vertebra (ib. fig. 5) shows the hinder concave
articular surface of the centrum, ¢, which is 2 inches 3 lines in dia-
meter. The margin of the concavity is thick and convex, as in the
dorsal vertebra (loc. ct. p. 414, pl. xvi. fig. 3) of the preceding paper
on Platypodosaurus. The neural canal, m, is 7 lines in diameter at
its hinder outlet, m. The neurapophyses, x, n, rise to 10 lines before
sending off the diapophyses, which are broad and flat above, and
give attachment to a slightly curved pleurapophysis, pl, 45 inches
in length and 9 lines in breadth; at its free end it almost comes
into contact with the iliac labrum.
Of all the examples of pelvic structures in extinct Reptilia which
have come under my observation, the type of pelvis exemplified in
Platypodosaurns departs furthest from any of the modifications of
that part of the skeleton known in existing Reptilia, and at the same
time makes the nearest approach to the Mammalian pelvis. This is
seen, not only in the number of sacral vertebre, but in their breadth,
due to the outward extension of their expanded transverse processes.
The Mammalian character is more marked by the breadth of the iliac
bones, and by the extent of confluence of the similarly expanded
ischia and pubes, together with their further confluence at the
ischio-pubic symphysis (which, though the bones are here fractured
in the present example, may be inferred to have existed from the
general resemblance of the pelvis of Dicynodon to that of Platypodo-
saurus).
The small solution of continuity between the ischium and ilium
shown by the foramen (0, fig. 2, Pl. X.) closely accords with the
foramen in a similar part of the pubis of many modern lizards, which
gives passage to the “superficial femoral artery.” It may, however,
if the ischium be actually continued into its periphery in Platypo-
dosaurus, be regarded as a trace of a “‘ foramen obturatorium.”
EXPLANATION OF PLATE X.
Platypodosaurus robustus,
Fig. 1. Front view of pelvis: + nat. size.
2. Side view of acetabulum, ischium, and pubis: i nat. size,
3. Back view of sacrum and iliac bones: +} nat. size.
4, Section of ilium anterior to the acetabulum: nat. size.
5. Back view of last lumbar vertebra: nat. size.
* Loe. cit.
270 PROF. OWEN ON THE SKELETON OF
Discussion.
Mr. Hurxe asked if the lateral view of the pelvis of Platypodo-
saurus really bore out the view of the author as to its remarkable
Mammalian affinities, and especially whether the acetabulum is in
front of or behind the vertical of the sacro-iliac Junction. He further
remarked that most reptiles have not one but many series of teeth ;
and such would seem to have been necessary for carnivorous animals,
in which the teeth are continually lable to damage. He stated that
the canine described in this specimen seemed different from what had
been described as characteristic of the order Theriodontia.
Prof. SreLey inquired whether the ilium of Platypodosaurus re-
sembled that of a Seal. So far as he could judge from the single
diagram, the whole pelvis closely resembled that of Dicynodon ; and
if so, its affinities with other orders of fossil reptiles were more 1m-
portant than its presumed analogies with the Mammalia. This type
of pelvis was approximated to by certain Dinosaurs, and, but for
their prolonged iliac bones, was even more closely paralleled by the
pelvis of some Solenhofen Pterodactyles. Even should the marsu-
pial bones suspected by Prof. Owen have existed, the character
need not be mammalian, since it is well developed in the Pterodac-
tyle group. ’
With regard to the Theriodontia, he was unable to admit the
importance of the characters and presumed characters on which
the order was founded. The teeth of existing Lizards would, by
the variety of types which they present, as well sanction ordinal
subdivisions as the Anomodontia. The Dinosaurs also, with their
carnivorous and herbivorous types of teeth, presented greater variety
among themselves than that which was held to separate the fossil
described from its Anomodont allies. He could not see how the
circumstance of the so-called canine tooth being better nourished
and growing larger could in these animals be an ordinal character.
He thought it premature to infer the absence of successional teeth
as an ordinal character—because the animals described were mature,
and succession of teeth may well have occurred in early life. Not
only were there no such characters dividing these animals from
Anomodonts as separate Crocodiles from Lizards or Turtles from |
Crocodiles, but there was absolutely no important difference of plan
in the structure of the skulls of Anomodonts and the so-called
Theriodonts. Prof. Owen had long ago classed these animals as
Cynodontia, forming a family of the Anomodonts; that classification
he thought excellent, but he could not accept the family as an order
or adopt its new name.
Mr. Twetverreers had just returned from the district of widely
spread Permian deposits of Russia. So far as he knew, these rocks
had only exhibited two types of Reptilian structure, the Labyrintho-
dontia and the Theriodontia. He asked for information as to the re-
lations between the latter and several genera described by Prof. Cope. -
Prof. Owen said that the sacrum of the Dinosaurs approached
that of birds rather than that of mammals. He was not aware of
AN ANOMODONT REPTILE. Dal
any Pterodactyle pelvis which resembled that of Platypodosaurus.
He admitted that the dentition of the Lizards varied, but asserted
that it never approached to that of the Theriodontia, in which the
teeth were not ankylosed to the jaw. He was not able to compare
these forms with the genera of Prof. Cope, in the absence of suffici-
ently large and detailed figures to illustrate the descriptions given
by that naturalist.
272 G M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
21. AppITIONAL OnsERVATIONS on the SUPERFICIAL Guotoey of BririsH
Cotompra and apsacENtT Reeions. By Groraz M. Dawson,
D.Se., F.G.S., Assoc. R.S.M., Assistant Director of the Geological’
Survey of Canada. (Read March 9, 1881).
ConrTENTs.
Observations on the Southern part of the Interior of British Columbia.
Observations north of the 54th parallel in British Columbia.
Peace and Athabasca Basins.
Additional Notes on the Coast.
Glaciation of the Queen-Charlotte Islands.
General Remarks and Conclusions.
In two papers previously communicated to the Geological Society,
the results of observations on the glaciation of the northern portion
of the American continent from Lake Superior to the Pacific have
been given*. The geological work of which these observations
formed a part was carried on first in connexion with the North-
American Boundary-Commission Expedition, and subsquently on the
Geological Survey of Canada. In continuing the exploration of
British Columbia on the Survey last named, during the seasons of
1877, 1878, and 1879, many additional facts of interest have been
gathered, which it is proposed here briefly to summarize and discuss
with special reference to the second of the two papers above men-
tioned, in which a description of the salient physical features of the
province of British Columbia has been given, and a map published ;
to these, which it is unnecessary here to repeat, reference should be
made in considering the points now brought forward.
Observations on the Southern part of the Interior of British Columbia.
In the more detailed examination of that part of the southern
portion of the province extending from the Fraser eastward to the
Gold ranges, and including the whole breadth of the region formerly
called the interior plateau, traces of a general north-to-south
glaciation have been found in a number of additional localities at
high levels ; and it would appear that the ice, whether that of a great
glacier or water-borne, pressed forward to, or even beyond, the line
of the 49th parallel, notwithstanding the generally mountainous
character of that part of the country. With the facts previously
recorded, these now extend the known area of north-to-south
glaciation to a portion of the plateau over 400 miles in length.
The most striking instance of this general glaciation, and that
which carries it up to a height greater than elsewhere observed,
is met with in the case of Iron Mountain at the junction of the
Nicola and Coldwater rivers. This mountain is one of the more
prominent points of that portion of the plateau, which, toward the
eastern or inland borders of the coast-range, becomes rough and
broken. It rises in a broad dome-like form to a height of 3500
* Quart. Journ. Geol. Soc. vol. xxxi. p. 603, and vol. xxxiv. p. 89.
—
BRITISH COLUMBIA AND ADJACENT REGIONS. 273
feet above the neighbouring river-valleys, or 5280 feet above the
level of the sea. Its summit has been heavily glaciated, the projecting
rocky masses being worn into ridges parallel to the direction of ice-
movement, the indicated direction of which is nearly parallel to a
bearing N. 29° W. to 8.29° E. If not due to the general glaciation,
these markings can have been caused only by ice from the coast-
ranges; and though ice has flowed from these as from the. other
mountain masses of the province during the later portion of the
elacial epoch, I believe the situation of Iron Mountain to be such as
to preclude altogether this mode of explanation. The mountains of
the coast-ranges are neither high enough nor so near as to supply a
body of ice capable of overriding it.
On the plateau south of Kamloops glaciated surfaces have been
found in several places at an elevation of about 3200 feet above the
sea. The locality is far removed from any mountain-ranges capable
of giving rise to extensive glaciers, being situated in the very centre
of the interior plateau. The rocks are broadly ice-shaped and not
unfrequently polished, more rarely distinctly striated. The direction
of movement varies from 8. 6° E. to 8. 27° E. On another part of
the plateau, north of the course of the upper part of the Nicola
River between Stump and Douglas Lakes, at an elevation of about
3622 feet, are glacial traces similar to the last, consisting of polishing
and striation without fluting, having a general direction of 8S. 9° E.
Still another instance of this general glaciation is found on the
eranite rocks near Chain Lake, between Lake Okanagan and the
Similkameen River, in latitude 49° 40’ N. Here, asin the cases before
mentioned, the circumstances seem entirely to preclude any expla-
nation by local glaciers, as the portion of the plateau on which it
occurs is fully up to the general level, and surpassed only by a few
insignificant hills at a considerable distance. The rock-surfaces
are beautifully polished, and show striation varying in direction
between 8. 20° E. and S. 28° E., but no deep grooving. The ele-
vation is 4075 feet.
The Okanagan valley has been alluded to in the paper already
referred to as the most important southern gateway of the interior
plateau. The bottom of this valley, where it crosses the 49th
parallel, is about 860 feet above the sea-level. It 1s wide, and must
at one time have been much deeper, as its rocky floor 1s not now seen.
It occupies the axis of a general depression of some magnitude, and
appears to have carried the drainage of a great part of the interior
of British Columbia at a former period. ‘This valley has probably
been subject to heavy ice-action during the time of general glaciation ;
but to what extent the features now found may bé due to this, and
in how far to a subsequent period when, as a narrow arm of the
sea or of a great lake, it carried southward ice produced by glaciers
nearer the mountains, it is now difficult to ascertain. Glacial
striation was observed descending obliquely from the sides toward
the centre of the valley, and also in several places in the valley
itself, but in both cases without distinct grooving. The rocks of
the sides of the valley are often distinctly moutonnées; and, as seen
274 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
from a distance, those on the lower part of the slopes show
flattened outlines, while those higher up are more abruptly rounded
and have not been so thoroughly ground down.
The general statements made in a former communication, in
reference to the covering of Boulder-clay or unmodified drift spread
over the entire area of the interior plateau, are borne out in the region
now more particularly in question. From the rearrangement of
this material the great systems of terraces subsequently mentioned
have been formed.
Details need not be given of the evidence in striation and rock-
polishing of the existence of glaciers radiating from the various
mountain-systems, though it may be mentioned that some of these
seem to have had a very great extension down the lower valleys.
In this southern portion. of the interior plateau, terraces are
exhibited on a scale scarcely equalled elsewhere. ‘They border the
river-valleys, and at greater elevations are found expanding beyond
these and attached to the higher parts of the plateau and mountains..
None has yet been found here, however, equal in height to that
previously described on [1-ga-chuz Mountain in the north at 5270
feet above the sea. Many of the terraces and “ benches” of the
valleys may be the result of the gradual cutting-down of the river-
course in the hollow previously filled with glacial débris ; but for others,
including more particularly those of the higher levels, no explanation
short of the complete flooding of the plateau-region will suffice.
Knowing therefore that the water must have stood successively at
every lower level, it is of comparatively little importance that in the
case of some of the lower terraces it becomes impossible to determine
whether they belong to this period of the retreating waters or to a sub-
sequent river-erosion.
In this region the terraces frequently surpass 3000 feet in eleva-
tion above the sea-level. The more prominent of those seen on the
southward slope of Iron Mountain may be taken as an example
of the arrangement of these old water-marks. These terraces are as
follows, the approximate heights being given in feet—2386, 3063,
3392, 3611, 3715. It is frequently observed, however, that the
occurrence of a terrace at any particular level is merely a matter
of local circumstance, probably dependent on the supply of material
and other such causes; and in different places not very remote the
the scale of terraces often differs. This is illustrated on Okanagan
Mountain, situated east of the lake of the same name. On the
south side of this elevation the principal terraces were baro-
metrically determined as follows—1862, 2042, 2141, 2645, 2800,
2839 feet; on the northern slope six principal terraces were again
observed, as follows—1451, 1579, 1962, 2452, 2553, 2879 feet.
The wide trough-like valleys which traverse the plateau are, over
a considerable portion of its extent in the southern part of the province,
partly filled with a deposit of white silt or loess-lke material com-
parable with that described under the same name in the Nechacco
basin to the north*. It is, however, unconnected with the latter,
3 * Quart. Journ. Geol. Soc. vol. xxxiv. p. 105.
BRITISH COLUMBIA AND ADJACENT REGIONS. 275
and at a considerably lower elevation, reaching a maximum height
of about 1700 feet above the sea. In the vicinity of Kamloops
Lake and in the South Thompson and Okanagan valleys, it is well
shown, generally forming the first terraces above the rivers. In
origin it is probably, like that of the Nechacco region, a deposit from
the turbid waters flowing from glaciers at a time when these had a
considerable extension from the various mountain-ranges. At this
time, either from general depression of the land, or the damming
of the valleys by ice or moraines, a system of winding water-ways,
lakes or fiords, must have occupied the main valleys. The heads of
these valleys in the Gold ranges still hold long and deep lakes, on
the banks of which, where they have been examined (more parti-
cularly in the Shuswap region), drift deposits are comparatively un-
important, and the white silts arenot found. The fine silty material
must have been deposited in somewhat tranquil waters; but it
appears difficult to explain its absence from the valleys on the
flanks of the Gold ranges. It may be suggested that the currents
in the upper parts of the valleys were so strong as to prevent
the deposition of the silt; but, apart from the difficulty found in
supposing such great bodies of water as the valleys must have held
at this time to be in rapid motion, there is no such sudden widening
in the valleys at the points at which the silt commenees as might
account for the slackening of the current.
It is perhaps on the whole most probable that the basins now
occupied by the Shuswap lakes and others in a like position were
filled with glacier-ice, from which the water flowed down the long
valleys, while the abrasion of the rocky beds of the glaciers supplied
in large quantity the material of the silt deposits. From the height
at which the silts occur, their greater coarseness in the lower part
of the Okanagan valley, and the evidence of current-action in that
valley near Osoyoos Lake, it is probable that this depression has
served as the main outflow of the white-silt lake or sound. At the
last 16 would appear that the glaciers retreated with considerable
rapidity, becoming extinct or dwindling to nearly their present
size, and leaving the upper portions of the valleys which penetrate
the Gold ranges almost free from débris and ready to form the
basins of the lakes which now generally occupy them.
The explanation here adopted to account for the existence of these
lakes will, I believe, be found applicable to many in other parts of
British Columbia, and is again referred to on a subsequent page.
It is the same advanced by A. Helland for Norwegian lakes *.
Whether any of the lakes in the region now in question lie in rock
basins of glacial formation has not been determined, as the valleys
below their outlets are generally filled to an unknown depth with
detrital materials.
Observations north of the 54th parallel in British Columbia.
An exploratory survey of the remote region lying between the
54th and 56th parallels in British Columbia and of part of the
* Quart. Journ. Geol. Soc. xxxiil. p. 165.
276 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
Peace and Athabasca river-basins to the east of the Rocky Moun-
tains, enables the characters of glacial evidence to be defined further
north, and has aided in the decision of some theoretical points
referred to in the sequel. Most of the facts observed to the west of
the Rocky Mountains resemble so closely those previously described
for the regions south and east of this that they do not require
lengthened notice. The southward or south-eastward passage of
glacier-ice in the valley of Babine Lake is indicated by glacial
grooving, while the valley of the Skeena has formed a main channel
of discharge of glacier-ice toward the coast. In the mountains
between the valley of this river and Babine Lake a somewhat irre-
gular, but still, I believe, distinct terrace-flat was observed on the
watershed at an elevation of 4800 feet. Its surface is strewn with
water-rounded stones differing from those of the mountains of the
vicinity. The region north-east of Stuart Lake, extending to
M‘Leod’s Lake and the Parsnip River at the base of the foot hills of
the Rocky Mountains, is deeply drift-covered, the surface consisting
either of Boulder-clay charged with erratics of varied origin, or
terrace-flats formed by its rearrangement. This region lies to the
north of and somewhat higher than the Nechaco basin, which is
characterized by the white silts of a former paper*. ‘The highest
part of its surface crossed by the trail has an elevation of 2900
feet.
In the valley of the Misinchinca, flowing westward from the
summit of the Pine pass of the Rocky Mountains, glaciation was
observed in a few places parallel to the direction of the main de-
pression. In the Pine-River valley, draining eastward and joining
the Peace, no glaciated surfaces were seen—a circumstance which
may arise from the comparatively soft character of the rocks.
Peace and Athabasca Basins.
In the comparatively level country drained by the Peace and
Athabasea rivers, to the north-east of the mountains, underlain
by unaltered rocks of Mesozoic and Tertiary age, the chief evidences
of the glacial period are found in the distribution of erratics, and
the existence of extensive “drift” deposits. In travelling eastward
from the mountains by the Pine-River valley, a remarkable absence
of such deposits is noted in that part of the valley which traverses
the eastern foot hills ; but at the Middle Forks the plateau, with an
elevation of 1000 feet above the river, or 3000 feet above the sea,
and at a distance of thirty miles from the indurated rocks of the
mountains, is strewn with rounded pebbles of quartzite &e. from
these rocks, though material of local origin preponderates. Highteen
miles further east, at the Lower Forks, the superficial deposits are
much more important, covering the surface of the plateau to a
considerable depth, and consisting of gravelly beds passing upwards
into finer silty materials; the elevation of the plateau is here 2350
feet. In continuing eastward after passing over a summit of 3300
feet on the line followed, Laurentian boulders which must have come
* Quart. Journ. Geol. Soc. vol. xxxiv. p. 105.
BRITISH COLUMBIA AND ADJACENT REGIONS. 277
from the axis of these rocks to the east or north-east were first ob-
served, and appear in abundance, at a height of from 2300 to 2500
feet, near the D’Echafaud River, in latitude 55° 45’, longitude 120°.
Kast of this point the wide Peace-River plateau extends, and the
general character of the country in regard to its superficial deposits
is so uniform that it is unnecessary to particularize localities in de-
scribing it. Its surface is so thickly covered that exposures of the
underlying rocks are, as a rule, found only in the larger river-valleys.
The lower layers of the drift appear to represent the Boulder-clay of
the great plains to the south and east and the northern part of British
Columbia to the west; they are sandy clays with boulders and ~
stones in abundance, and their upper surface is somewhat irregular,
rising in some places in ridges or broad gentle elevations, which
stand out above the newer silty deposits in which a great part of
the surface is enveloped. ‘The silt is generally pale grey or fawn-
colour, and while in places passing almost into clay, becomes occa-
sionally a fine sand. This sandy covering of the surface is found
especially at the southern rim of the Peace basin, near the Atha-
basca, where the plateau attains an elevation of about 3300 feet
(long. 117°). The ridges at this elevation are still thickly strewn
with Laurentian boulders.
In regard to the material of the drift, the stones and boulders
scattered over this great district are, in part, those of the Rocky Moun-
tains to the west, in part derived from the Laurentian axis to the
north and east. ‘The fragments from the first-mentioned source are
generally of quartzite; the limestone and other softer rocks accom-
panying these in abundance in the vicinity of the mountains, de-
creasing rapidly as we recede from them. The Laurentian mate-
rial is chiefly gneiss and granite of the usual well-marked types.
Between the Athabasca and Saskatchewan (long. 113° 30’) the
plateau attains a maximum elevation of about 2300 feet, and
Laurentian boulders are everywhere exceedingly numerous.
Additional Notes on the Coast.
In the fiords penetrating the coast of the mainland of British
Columbia, and channels intervening between the numerous islands
lying off it, from the southern extremity of Alaska to the north end
of Vancouver Island, marks of the passage of glacier-ice are to be
found wherever the rocks are unweathered (see Map, p. 278). These
marks are generally in strict conformity with the directions of the
passages, which it is evident must have been filled with ice moving
in the main seaward from the coast-ranges, in which many smaller
glaciers are still found. Whether at any time the supply of ice has
been so great as to form a confluent mass flowing toward the sea, at
right angles to the general direction of the coast mountains, and with-
out regard tothe smaller features of the surface, has not been definitely
ascertained ; but it is highly probable that this has happened. The
outer islands of the Shore archipelago have scarcely been examined ;
but the little group called the Gnarled Islands (lat. 54° 39’), on the
south side of the strait, thirteen miles wide, which lies between
Q.J.G.S. No. 146. U
278 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
Dundas Island and Cape Fox at the southern extremity of Alaska,
shows heavy grooving from N. 50° E. to 8. 50° W., proving that
this strait must have been filled with ice.
Sketch Map of part of British Columbia, showing the supposed exten-
sion and general direction of flow of the glacier-ice when near its
maximum limit.
32°
USAMA
Fd ME Vii
ra € y
TuwHa Naga!
SQNV1St a.t/Lo
~S ud
KA oho vtlll lll
SAIS SYD VAI
AIT IAAT IT SSE
The arrows indicate the direction of flow of the ice.
The dotted line shows the seaward margin of the confluent glacier.
The scarcity of examples of well-marked terraces on the coast,
and the comparatively small elevations at which they are found, has
been remarked previously. At Fort Simpson, however, in lat. 54°34’,
the surface bears a considerable thickness of detrital matter, and from
a distance this appears to form an ill-defined terrace at a height of
somewhat over 100 feet. A few miles further southward, at Metla-
katla, there is a well-marked terrace, flat, with an elevation, baro-
metrically determined, of 95 feet above high-water mark.
In the previous paper, already several times referred to, evidence
was brought forward in favour of a belief that during a part of the
glacial period a vast glacier filled the entire Strait of Georgia, which
separates the south-eastern part of Vancouver Island from the main-
land, and that the ice swept across the south-eastern extremity of the
BRITISH COLUMBIA AND ADJACENT REGIONS. 279
island, and may even have passed some distance southward to Puget
Sound, and westward by the Strait of Fuca. It still remained, how-
ever, to determine whether the ice supply of this glacier was wholly
derived from the neighbouring mountainous country, or whether (as
might be supposed in accordance with some theories of glaciation) a
great ice-sheet entered at Queen-Charlotte Sound, and passed con-
tinuously southward between it and the mainland. Itis now found
that the last-mentioned idea must be abandoned. In several places
about the northern end of Vancouver Island, but more particularly
on the little islands of the Masterman group near Hardy Bay, and
on those in Beaver Harbour, are marks of very heavy glaciation
from south-east to north-west, in bearings varying from N. 49° W.
to N. 62° W. This not only passes over the islands, but has grooved,
polished, and undercut vertical, or nearly vertical, faces on their south-
eastern parts, while the north-western slopes are comparatively rough.
These traces precisely resemble those found in the track of the
Strait-of-Georgia glacier near Victoria*, and show that here, as
there, the ice rode over the low extremity of Vancouver Island.
The seaward margin of the continental shore is here also low, and
the width of the glacier of Queen-Charlotte Sound can scarcely have
been less than twenty or twenty-five miles, and may have been much
greater.
Some additional evidence of the movement of the upper parts of
the Strait-of-Georgia glacier has been found at Nanaimo, on the
inner coast of Vancouver Island, sixty miles north-west of Victoria.
Hard sandstone rocks which have been bared on the colliery railway
show heavy glacial grooving running parallel to the general trend
of the coast and Strait of Georgia in such a way as to prove that
the entire strait must here also have been filled with ice. No
local glaciation, which would radiate from the mountains of the
district, can account for the facts. In clays resting on these gla-
ciated rocks, shells like those formerly observed at Victoria were
found, a small collection comprising Sawicava rugosa, Mya truncata,
and Leda fossa. The height of the locality is about 70 feet above
the sea.
Between Vancouver Island and the mainland, on both sides of
the central region from which the ice spread in two directions to
form the Queen-Charlotte-Sound and Strait-of-Georgia glaciers, well-
stratified deposits of clays and sands occur, in some places forming
cliffs 200 feet in height. In the course of the Queen-Charlotte-
Sound glacier, Cormorant Island may be cited as an example of
these deposits ; and in that of the Strait of Georgia, Harwood, Mary,
Hernando, and Savary Islands. These deposits resemble those of
Victoria, New Westminster, and the islands in the southern part of
the Strait of Georgia previously described, but imply for the period
of their formation a decreased length in the glacier, from its point of
maximum extension, of at least 100 miles. Harwood, Mary, Her-
nando, and Savary Islands lie about the entrance of Bute and
* Quart. Journ. Geol. Soc. vol. xxxiv. pp. 94, 96, 99.
v2
280 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
neighbouring inlets in such a position as to suggest that they may
in part represent a moraine marking a stage in retreat of the ice.
They form the projecting points of a comparatively shoal bank off
these inlets, which, in their upper parts, are very deep. Boulders
here occur in great abundance on the beaches, and are probably
derived from a Boulder-clay or morainic material underlying the
well-bedded deposits.
Glaciation of the Queen- Charlotte Islands.
These islands were the subject of geological examination in 1878.
They form a compact archipelago widely separated from the southern
extremity of Alaska to the north, and the western coast of British
Columbia to the east, and may be regarded as a partly submerged
mountain system, the axis of which lies in a N.N.W.-S.S.E. bearing.
In its central part summits surpassing 4000 feet, and still bearing
patches of perennial snow, are frequent, but it falls at both ends.
On the north-east side of the mcuntain axis, at its north end, is a
wide triangular attachment of flat land forming the greater part of
Graham Island.
In these islands we find everywhere evidence of the descent of
glacier-ice from the mountains toward the sea, but (with one im-
portant exception subsequently noticed) none of the passage across
the group of any more ponderous ice-mass. The channels and fiords
penetrating the southern portion of the islands show in general di-
stinct and heavy glaciation which has evidently been local in cha-
racter, the scoring and grooving being parallel to the main directions
of the valleys, and changing with their course. In Houston-
Stewart Channel, separating Prevost and Moresby Islands, the ice
has evidently flowed from the axial mountains both eastward and
toward the open Pacific to the west. Many of the boulders of the
beaches are distinctly glaciated, and, as they lie in some places rudely
packed together, seem to have been little disturbed since they were
deposited by the ice. Sands, clays, and other detrital deposits re-
ferable to the period of glaciation are here almost entirely wanting,
and the water round the coast is deep.’
Further north, near Laskeek, where the width of the islands
becomes greater, there is evidence, i in the comparatively slight de-
gree in which the rocks at the outer ends of the inlets are slaciated:
that the glaciers did not long stretch much further out than the pre-
sent coast-line. At Cumshewa Inlet (lat. 53°), and further north at
Skidegate Inlet, the character of the coast changes, becoming low;
but both these inlets still head in the high axial mountains of
the group. ‘Traces of the glaciers of these inlets are found nearly
to their mouths ; but while the upper parts are still deep and fiord-
like, they are partly blocked at their seaward extremities by trans-
verse bars, and shallow water extends far off shore.
Further north a series of fiord-like valleys are still found pene-
trating the eastern side of the mountainous axis of Graham Island,
and the shoal-water found off Cumshewa and Skidegate is repre-
BRITISH COLUMBIA AND ADJACENT REGIONS 281
sented by the wide stretch of flat land before alluded to. Several
of the fiords here open together into a large sheet of water forming
the upper part of Masset Inlet, which communicates with the sea to
the north by the long narrow passage known as the Masset Sound.
The fiords are heavily glaciated, bordered in most places by steep
rocky shores, deep and free from drift deposits, and contrast in these
respects markedly with the low-shoal eastern shores of the Masset
expansion into which they open.
The composition of the low land to the east and north-east is
best shown in the cliffs forming its eastward-facing margin. A few
miles north of Skidegate a low cliff or bank shows deposits which
are evidently of glacial age, cut off above by a gently undulating
surface of denudation, above which is 10 or 15 feet of material
which shows no sign of blending with that below. The upper de-
posit consists of sand and well-rounded gravel in regular and often
nearly horizontal layers. It has here become in many places quite
hard, being apparently cemented by ferruginous matter. Its lower
layers hold small boulders, a few of which are from 18 inches to 2 feet
in diameter. The lower deposit in one place is a typical Boulder-
clay, with many half-rounded or subangular stones and occasional
boulders of some size. The matrix is bluish grey, hard, and some-
what arenaceous, the whole being irregularly mingled, and having
no distinct bedding. Ata short distance this Boulder-clay begins
to show bedding, and to become interleaved with hard clayey gravels
composed of well-rounded pebbles. The stratification of these is
undulating and rather irregular, and there is some local unconformity
by erosion between the different layers. A few paces still further
on these become interbedded with, and are eventually replaced by,
hard, bluish-grey, arenaceous clays, which hold some pebbly layers
and an abundance of broken specimens of mollusks, among which
Leda fossa is the most common. A small Cardium-like shell and
fragments of a Balanus were also observed.
Further north on this coast the clays, with the overlying sandy
deposit in greater or less thickness, form long ranges of cliffs ; and
though locally irregular, their general character continues the same.
The clays are, in some places, very hard, and were observed to hold
fragments of trees quite brown in colour, but not mineralized.
These deposits, as a whole, very closely resemble those previously
described as occurring at Victoria, on the south-eastern extremity
of Vancouver Island.
Lying like Masset Inlet near the junction of the hilly and low
countries is Naden Harbour, and between this and Masset Inlet are
two large freshwater lakes, which doubtless occupy an analogous
position, but have so far not been visited by any but Indians.
Southward there is reason to believe that there are one or more
basins in a similar relation between Masset Inlet and Skidegate.
Boulders are very numerous on the coast of some parts of the
northern portion of Graham Island; and these and the beach-
gravel are in many cases formed of rocks which must have been
transported from the mainland to the north or east, and quite unlike
282 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
those of the Queen-Charlotte Islands. Similar erratics appear to
characterize in greater or less abundance the whole of the low
country above described, but are not found about the heads of the
south-western extremities of Masset Inlet.
It has previously been shown that at the time when the Strait-of-
Georgia glacier began to diminish the sea must have stood consider-
ably higher in relation to the land than at present, and the glaciated
rock surfaces about Victoria and Nanaimo no sooner appeared from
beneath the glaciers than they were covered by deposits holding
marine shells. Such must have been the state of affairs also in the
Queen-Charlotte Islands ; and to this time are doubtless to be referred
the clay and sand deposits of the low north-eastern part of Graham
Island above described. The material of these must have been sup-
plied from the glaciers of the islands themselves, but added to also (as
the nature of the boulders proves) by the debris borne on floating ice
from the larger glaciers of the mainland, the sea levelling and
spreading abroad the material, and preventing the formation of any
well-marked terminal moraines by the island glaciers. The rocky
beds of the fiords and Masset-Inlet expansions must have been shaped
to some extent by the ice; but the absence ef drift material from their.
areas, and especially of the erratics derived from the mainland, are,
with their situation, good reasons for supposing that they mark the
regions last covered by glacier-ice, and from which it eventually re-
treated with some rapidity, leaving the hollows formerly occupied
by it to become first inlets, and then, with increasing elevation, in
some instances lakes.
The exceptional case which seems to show the impingement on the
Queen-Charlotte Islands of ice not produced on them was found on
the north coast on the little islands lying outside the entrance to
Masset Inlet; but it is probable that similar traces might be found
by search in additional localities in this vicinity. Wider exposures
of basalt a few feet above high-water mark here show very heavy
though somewhat worn glaciation in a direction 8. 10° E., or N.
10° W., but probably the former. The depth and parallelism of the
grooving would appear to show that it is glacier work. The moun-
tainous axis of the islands in this their northern part does not ex-
ceed in height about 1300 feet, and where nearest is about 15
miles from the locality, while the direction of the marking is not
that which would be followed by ice descending from the mountains
under any circumstances, being more nearly parallel to than radiant
from them. It is, however, just that which ice-masses floating up
or down the strait separating the islands from the mainland must
have taken, or glacier-ice pushing southward from the long fiords
of the Prince of Wales group in Southern Alaska, sixty miles
distant. It may, I believe, be attributed with greatest probability
to the last-named agent; and in view of the great extension which
the glaciers of other parts of the coast must at one time have had,
that required for the Prince of Wales group and adjacent channels
does not appear excessive.
BRITISH COLUMBIA AND ADJACENT REGIONS. 283
General Remarks and Conclusions.
It is somewhat difficult to connect the various observed facts of
the glaciation of British Columbia in a general theory of glaciation,
owing to the complexity of its physical features and their marked
character. Several conjectural schemes were advanced in a former
communication ; but, abandoning the seemingly untenable theory
of a great polar ice-cap, two probable hypotheses appear to remain.
A general north-to-south movement of ice is indicated by striation
in a number of places in the central-plateau zone, extending now
for a length of over 400 miles. This region, from elevations ex-
ceeding 5000 feet downward, is also covered thickly with drift-de-
posits requiring, by their character and mode of arrangement, the
action of water. ‘To account for these facts it was thought that
either the flow of strong arctic currents bearing heavy ice during a
period of great submergence might be supposed, or that the whole
region may have been buried under a massive confluent glacier, the
drift-deposits being laid down as it retreated in the water of the
sea during a period of subsidence, or in that of a great lake held
in by glacier-dams in the valleys of the several mountain-ranges.
It was presumed that the gaps of the Peace and Pine rivers in the
Rocky-Mountain range might have sufficed for the entrance from the
north-east of such currents and masses of ice as would be required
by the first theory; but the examination of the region, with this
supposition in view, has convinced me that, notwithstanding the
general decrease in elevation and width of the Rocky Mountains,
the valleys of the rivers are too narrow and indirect, and the sur-
rounding mountains too high, to allow the inflow of sufficient cur-
rents with the degree of subsidence which would be required by
most of the localities of glaciation and by the superficial deposits.
Neither is there any evidence of the passage of drift-material in this
region across the mountains either from east to west or in the oppo-
site direction.
It therefore appears to remain as the most probable hypothesis
that a great glacier mass resembling the inland ice of Greenland
has filled the region which may be called the Interior Plateau, be-
tween the Coast Mountains and the Gold and Rocky Mountain
ranges, moving (though perhaps very slowly) southward and south-
eastward from the region of great precipitation and high mountains
of the northern part of the province*, and discharging by the
Okanagan depression and through the transverse valleys of the
coast range. It still appears to me most probable, however, that
this stage of the glacial period was closed by a general submergence,
during which the deposit referred to as Boulder-clay was laid down
in the interior plateau, and that as the land again rose it assumed
its present terraced character. Conditions may bé suggested to
account for the temporary existence of a great lake in the interior
* Explorations in the northern part of the province in 1879 have shown
that the mountains here are even higher and more extensive than had been
supposed, several ranges exceeding 8000 feet in great portions of their extent.
284 G. M. DAWSON ON THE SUPERFICIAL GEOLOGY OF
plateau of British Columbia; but this will not explain the great;
height to which water-action has extended on the east side of the
Rocky Mountains*, which was probably synchronous. The last
stage of the glacial period in the northern part of British Columbia
appears to have given rise to the silts of the Lower Nechacco basin,
while on the opposite side of the Rocky Mountains similar deposits
were laid down over the Peace-River country, the elevation of the
two districts being nearly alike.
The general question of the origin of the drift-deposits of the
Great Plains having been fully discussed elsewhere?, it will be
unnecessary here to enter into it at length. The most remarkable
feature of the glacial deposits of the plains is the Missouri Coteau,
which it was supposed ran northward from the region near the 49th
parallel, where it was more particularly studied, nearly following
the margin of the third prairie steppe. This supposition has since
been in great measure confirmed ; and on the journey from Edmonton
to Winnipeg, in the autumn of 1879, I was able to examine cur-
sorily the character of this feature where it touches the north
Saskatchewan near the ‘“‘ Klbow,” and to observe the great accumu-
lation of heavy boulders of eastern and northern origin in that
vicinity. Further north, the facts now advanced show that with
the general lowering of the surface of the country the well-defined
zone of drift-deposits known as the Coteau is more or less completely
lost, the material being scattered broadcast over the upper parts of
the basins of the Peace and Athabasca rivers, and approaching in
considerable mass the highlands near the base of the Rocky Moun-
tains.
Over the whole western portion of the plains, from the 49th to
the 56th parallels, there is a mingling of the eastern and northern
Laurentian débris with that from the Rocky Mountains to the
west, the latter consisting largely of certain hard quartzite rocks,
and the overlap seeming “to imply the existence of a sea in which
ice derived from both sources floated freely.
Discussion.
The Presipent spoke of the care with which Dr. Dawson con-
ducted his researches, and the value of his observations.
Mr. Baverman stated that he was not acquainted with the district
described by Dr. Dawson; but he thought, from what he had seen
in Oregon and the Columbia valley, that many of the conclusions of
Dr. Dawson could be established. He, however, doubted whether
the ice had been quite so widely spread as Dr. Dawson supposed.
He described some of the great terraces on the Barrier River ; there
were sixteen, one over the other, on a stupendous scale. He had
traced them on the Columbia River to 2300 feet above sea-level ;
* Quart. Journ. Geol. Soc. vol. xxxi. p. 618.
+ Quart. Journ. Geol. Soc. vol. xxxi. p.603. ‘Geology and Resources of the
49th Parallel,’ p. 6.
————
BRITISH COLUMBIA AND ADJACENT REGIONS. 285
and they could be found still higher but for the degrading action of
the climate. The rapid melting of the snow, followed by freezing,
and slipping of the ice then formed, produced well-defined ice-
scratches in a very short time.
Prof. Boyp Dawxins said that he had studied the glacial phe-
nomena in America, though he had not been so far north; and,
so far as he could form an opinion, that northern area appeared to
have been a great area of dispersal of ice. In the Western and.
Pacific States, however, there was no evidence of a great ice-sheet,
only a rather larger extension of local glaciers. On the eastern side
the southern boundary of the confused glacial deposits, or the
drift, passed from the latitude of New Brunswick in a N.W. direc-
tion towards the area of the Mississippi, forming a low range of well-
marked hills. To the south of this are the ‘‘ Champlain terraces”
and traces of local glaciers on the higher hills. So that in North
America there are two great systems of glaciation—one in the N.W.,
such as Dr. Dawson had described ; and another in the N.E. region,
apparently pointing towards Greenland and Labrador.
286 T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
22. The Prrmtan, Triassic, and Liasstc Rocks of the Cartistx Basin.
By T. V. Hotes, Esq., F.G.S8. (Read February 23, 1881.)
[Puate XI. ]
IT am enabled, by permission of Prof. A. C. Ramsay, Director-General
of the Geological Survey, to lay before you the general results of
the Survey examination of the, Permian, Triassic, and Liassic rocks
in the country bordering the Solway Firth; but I do not propose
to discuss here the glacial drift and other superficial beds by which
the surface of the ground is almost entirely covered, and which are
the main hindrance to an understanding of the rocks which form
my subject this evening.
Papers on the Permian and Triassic rocks of the North-west of
England have been read before this Society by Prof. Sedgwick, by
Sir Roderick Murchison and Prof. Harkness, and by Mr. E. W.
Binney. But as few districts promise less, except as regards drift
and peat-mosses, than that immediately around the Solway, it has
hitherto been dealt with, as awhole, in a brief and cursory fashion.
In addition, a knowledge of certain borings, the results of which are
by no means generally known, is absolutely necessary to a correct
view of the structure of the Carlisle basin (see Map, Pl. X1.).
The lowest bed with which we are here concerned is the great
brick-red Upper Permian sandstone, so well shown at St.-Bees
Head, and named, therefore, the St.-Bees Sandstone. Between
St.-Bees Head and Maryport the coast consists of the underlying
Coal-measures, the St.-Bees Sandstone having been swept away by
marine denudation. But at Maryport it again becomes visible, its
most northerly appearance being below Swarthy Hill, on the fore-
shore, about midway between Maryport and Allonby. North of
Swarthy Hill none but superficial beds are exposed on the southern
shore of the Solway. On the Scottish side St.-Bees Sandstone appears
at Tordoff Point; but, with this exception, a walk along the coast
between the Sark and the Nith shows no more than one between
Allonby and Rockcliff, on the southern side. At a distance of one,
two, or three miles from the coast-line, however, Scotland has de-
cidedly the advantage, the corresponding part of Cumberland being
entirely destitute of sections.
Turning eastward from Maryport, the St.-Bees Sandstone is found
to occupy a belt of country ranging towards Dalston on the Caldew —
and Wetheral on the Eden. Between Maryport and the Caldew
its southern boundary consists of Carboniferous rocks of various
ages; and between the Caldew and the Eden of Lower Permian
beds. The Carboniferous-Permian boundary is almost invariably a
faulted one; in Shalk Beck, however, the unconformity between
the two formations is very distinctly shown about a mile above
Kast Curthwaite. The boundary between the St.-Bees Sandstone
and the Lower Permian beds, between the Caldew and the Eden,
Quart. Journ. Geol. Soc. Vol. XXXVIE Fi. X7.
S
BILE BES PREM
SAGs RS
ee. *
Reference.
| Sr i a
| S =. Las = WE ee Shiites
~
S hau i F
| 3 SS Stance Marls = Feral S¢ Beas Sandst.
S Ksridinton a
& EST sandstone. l= wee
S \
SP Ge borsterqns Rocks
| re) Lil of varus Ages.
—— Fazltis.
The mark ———— 1 om the downthrow Side.
0.4.8 Outlier of Kirklton Sandst.
; Fea Daj afall La landon,
SLE BASIN.
i
i Re ateaNA
s
4
4
+
any A
Bynes
5 a
+
Con
Fd
\
Guart, Journ. Geol. Soc. Vol, XXXVIE Pl. XI
0. Mi
Gases
Southerness
MARYPOR
tle
Se
oy
7
Sy
/
Sloth
ADUEV |
4
ye
L
ia
i
Ii
G
L hand? | A EN
Hf). wale L
b ifiT® Bangin gel : i
[ee —— eS}
Stanwie Marls
Aarklinten
| Sarudstone .
—— Faults.
BASIN.
Reference.
The mark —~— 1s on the downdrow Side.
O.K.S=Outher of Kirklixton Sandst.
|
3 eA Preis Shales
{EEE se Boas Sando
Lasers Shales
Perk Sindst.
Jy] Garbonuterous Rocks|
of runs Ages
CARS. PE)
Fred® Daniyerfotl bith, London.
SHOWING THE ROCKS OF THE CARLISLE
(Disregarding Superlfiaal Beds.)
Seale __{__{ i _# Hfiles
LIASSIC ROCKS OF THE CARLISLE BASIN. 287
consists of two great faults, which abut against each other at New-
biggin, on the Petterill. Both faults have a downthrow to the north.
The more westerly ranges from a point alittle north of Rose Castle,
on the Caldew, to Newbiggin ; the other from Newbiggin to Bracken-
bank, on the Eden, about two miles above the railway bridge at
Wetheral. This Brackenbank and Newbiggin fault is known to
exist for many miles eastward of the Eden; it has also (as I believe)
a considerable extension westward, in the direction of Cummers- |
dale.
The Lower Permian beds which are cut off by these faults are
the Penrith Sandstone, a bright red rock remarkable for the scale
on which it is false-bedded, and a red shaly series overlying it, and
directly underlying the St.-Bees Sandstone. The Penrith Sandstone
is well shown in the Petterill, a little below Wreay Bridge. The
junction of the Penrith Sandstone with the overlying shaly beds (which
in this locality contain gypsum) may be seen in the little streamlet
which runs into the Petterill from the east, after crossing the Car-
lisle and Penrith road about midway between Springfield and Carle-
ton Hill. A little lower down the Petterill, but just above the road
from Newbiggin Bridge eastward, there is a quarry in St.-Bees
Sandstone.
North of the faulted line the St.-Bees Sandstone is the only Per-
mian rock seen*. About Brampton it occupies a broad belt of
country between the Carboniferous formation on the east and the
Triassic rocks on the west. In the Eden it is well shown between
Brackenbank and Wetheral Bridge, and thence as far down as the
junction of the Eden and Irthing. In the Hether Burn, the Line,
and Cardwinley Burn sections are very abundant. In the Line the
full thickness of the St.-Bees Sandstone does not appear, owing to
Carboniferous rocks being brought in by a fault close to Brackenhill
Tower, above which spot no Permian beds are seen; but in the
Hether and Carwinley Burns there is an almost continuous series of
sections, from Carboniferous rocks below the St.-Bees Sandstone to
the Triassic beds above it. In both streams (as in Shalk Beck) a
thin breccia is seen at the base of the Permian formation, and there
is no fault at the junction with Carboniferous rocks. In the Esk,
north of the railway bridge between Scots Dyke and Riddings junc-
tion stations, the St.-Bees Sandstone may be seen, on the right bank
of the stream, on both sides of the Border-line; it also appears
in Moat Quarry and the cliff on the south side of the railway
between Moat Quarry and the ancient fortress known as Liddel
Strength. West of the Esk it is visible in the neighbourhood of
Scots Dyke, both in the Glinger Burn and Sark ; alsoin many parts
of the Kirtlewater, south of Kirtlebridge. It is well shown in the
railway-cutting on the north side of the road from Annan to Kirtle-
bridge, in the Annan water about Annan, and at Tordoff Point
on the Solway.
The dip of the St.-Bees Sandstone, which varies, as a general rule,
from north to north-west between Maryport and the Caldew, slowly
* Except a very thin breccia at its base.
288 T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
changes between the Caldew and Hether Burn, till, in the latter
stream, it is about south-west. It retains this (general) south-
westerly dip as far as the Esk, but west of it the dip becomes more
or less east of south. At Annan it is nearly due south.
No signs of the Lower Permian formations are visible east of the
Annan Water. It is somewhat singular, however, that the Permian .
rock between the Nith and Lochar Moss, in the neighbourhood of
Dumfries, is precisely like the Penrith Sandstone in appearance. It
is remarkable for the hardness and thickness of the beds of breccia
it contains. The two great Permian sandstones of Penrith and St.
Bees are so distinct in character, that there is usually no difficulty
in distinguishing them even in hand specimens.
Having traced the St.-Bees Sandstone around the circumference
of the Carlisle basin, except where prevented from doing so by the
waters of the Solway, the overlying beds now demand attention.
First of these come the Gypseous Shales of Abbey Town and Bow-
ness. So thickly and persistently covered by drift is the country
immediately around those two places that were the only informa-
tion obtainable that to be derived from natural sections the exis-
tence of the Gypseous Shales would remain entirely unknown ; nor,
indeed, would there be any reason to suppose the St.-Bees Sandstone
to be overlain in that quarter by any thing but glacial drift, peat,
and alluvium.
Fortunately, however, two borings come to our aid, one of which
discloses the fact that in the neighbourhood of Abbey Town more
than 700 feet of Gypseous Shales rest upon St.-Bees Sandstone, and
are themselves covered by nearly 200 feet of drift. The other
boring was made near the west end of Bowness, at high-water mark,
and proves the presence there of 367 feet of Gypseous Shales below
41 feet of drift. It is not absolutely certain that the Bowness
boring penetrated to the St.-Bees Sandstone, though it ended in red
stone; but it is very highly probable that such was the case, St.-
Bees stone being visible a short distance to the north, on the Scottish
shore. At Bowness, therefore, the outcrop of the Gypseous Shales
is beneath the Solway ; east of Bowness it probably ranges, under
water, in the direction of Rockcliff Marsh. Towards Silloth, on the
other hand, it is most likely outside the present coast-line, against
which it may abut in the neighbourhood of Allonby.
The southern outcrop of the Gypseous Shales can only be approxi-
mately traced across an entirely drift-covered country by the help
of the most northerly exposures of St.-Bees Sandstone. Its general
direction is from Allonby to West Newton, and thence to Wigton
and Dalston.
East of Bowness and Abbey Town, the only evidence bearing on the
existence of the Gypseous Shales is the record of an old boring near
Great Orton, to which I shall have again to refer in treating of the
Lias. It was made in search of coal in the year 1781. Below rock
evidently Liassic was “ red stone or clay sometimes mixed with vems
of white.” This description fits the Gypseous Shales very well, the
gypsum in them being in the form of thin lamine, and beds of any
=
LIASSIC ROCKS OF THE CARLISLE BASIN. 289
thickness being absent. On the other hand, in no other formation
at all likely to be found underlying the Lias at Orton would “ veins”
of a white substance be found.
But if the Gypseous Shales are neither seen nor recorded as
haying been bored through east of Great Orton, it may be asked
why I have treated them as older than the formation which directly
overlies the St.-Bees Sandstone north and east of Carlisle. On this
point the evidence certainly leaves something to be desired, though
there seems to me to be no doubt on which side the balance inclines.
As will shortly be seen, the bed in question (which I have called
the Kirklinton Sandstone) rests unconformably on that of St. Bees;
while there is neither evidence nor presumption of any kind in favour
of the existence of unconformity between the St.-Bees Sandstone
and the Gypseous Shales. Again, the presence of gypsum is, so far
as it goes, a presumption of Permian affinities, gypsum being found,
as | have already mentioned, in the shales underlying the St. Bees
stone, while it is not seen in any of the higher beds of this district.
Leaving the almost sectionless district west of the Caldew and
Eden till the time comes to treat of the Lias, it will now be most
convenient to discuss the sections seen in the first-named stream
about Dalston and Cummersdale.
St.-Bees Sandstone is visible on the Caldew at Brackenhow and
Buckabank, and here and there nearly as far down the stream as
the outfall of the Pow Beck at Dalston. Opposite Dalston Hall
the trap dyke, well known at Barrock Fell and Armathwaite, is
slightly shown on the right bank, at the spot at which river and
railway begin to run side by side. ‘This is the most westerly expo-
sure of this dyke in Cumberland; but as I am informed by Mr. J.
G. Goodchild that there is no ground for supposing (judging from
his knowledge of it in the Eden-valley district) that it is also a fault
of any magnitude, if a fault at all, I need say no more about it
here.
A few yards below the dyke, and on the same bank of the river,
is a low cliff of greyish sandstone, and it seems to me that in this
grey rock we probably have the uppermost beds of the St. Bees. The
borizrg near Abbey Town shows that directly below the Gypseous
Shales, and above the typical St.-Bees Sandstone, are about 40 feet
of sandstone and sandy shale, mainly grey in colour. No sandstone
like this is seen higher up the stream, and the rock next seen below
at Cummersdale is evidently not St.-Bees Sandstone at all. In
addition, Mr. J. G. Goodchild considers the beds at and below
Buckabank to be higher beds in the St. Bees than any he has seen
in the Eden-valley district, where the uppermost are cut off by the
Penine fault. .
The next section, that adjoining the rifle-butts at Cummersdale,
disappoints any expectations that may have been formed of at last
seeing the Gypseous Shales. Strange to say, they are nowhere visible
at the surface. The rock at the rifle-butts is a very soft, red, shaly-
looking sandstone, without any sign whatever of the presence of
gypsum. Similar rock may be seen here and there in the river-
290 T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
bank, as far down as Cummersdale Print-Works. It is, in short,
the Kirklinton Sandstone; but the dip at the rifle-butts is slightly
west of north, and, being towards the Caldew, the surface of the
low river-cliff is wet and slimy, and the characteristic bright colour
and false bedding are both obscured. The soft Kirklinton stone,
however, invariably weathers, as at Cummersdale, about, and for a
few feet above, the surface of the river, along whose course it is
exposed. A comparison of the sections at Cummersdale with those
about Kirkandrews-on-Esk and elsewhere will show this very
clearly. Fortunately the identity of the rock at Cummersdale is
placed beyond dispute by the presence of a small but dry section
about 100 yards below the rifle-butts. The spot is marked by the
stump of an old tree, at the base of the bank bounding the alluvial
flat on the right side of the stream. Here the bright and almost
scarlet: colour and false bedding are both manifest.
The question arises, in what way the absence of the Gypseous
Shales at Cummersdale may be best accounted for. There can be
no doubt that they suffered very much from denudation before the
deposition of the Kirklinton Sandstone, as their total absence east of
Carlisle bears witness. As regards the amount of their extension
eastward, there are but two items of evidence. ‘The first is the old
boring at Great Orton, already alluded to, in which 132 feet of what
were probably Gypseous Shales were pierced and (apparently) their
base not reached. ‘The second is a very recent boring at Justice
Town or Iinehow, about a mile above the junction of Line and Hsk.
This showed about 170 feet of Kirklinton stone resting directly on
that of St. Bees. ‘'hese borings tend to show that the Gypseous
Shales cease to exist more speedily north than south of Carlisle. On
the whole, I am inclined to think that the Gypseous Shales would be
visible at Cummersdale, but for an extension of the Brackenbank
and Newbiggin fault. ‘This, if prolonged westward, might very well
cross the Caldew between Dalston Hall and the rifle-butts, cutting
off the Gypseous Shales and bringing in the Kirklinton Sandstone
on its northern side; just as further eastward we find it bringing
down the St.-Bees Sandstone on its northern side against the Lower
Gypseous Shales on the south.
The Kirklinton Sandstone is best seen in the parish from which
it derives its name, and at Rockcliff and Netherby. I have already
described its appearance at Cummersdale. Descending the Caldew
it is again visible at Holmhead Bridge. Below Carlisle the upper
beds are well shown at Skew Bank, north of Grinsdale, and lower
ones at Rockcliff. Ascending the Eden from Carlisle it appears at
Rickerby, in the river-bed at Low Crosby, and in the left bank a
few yards N.E. of Holmgate. Thejunction with the St. Bees stone
must be between the last-named spot and the junction of the Kden
and Irthing.
Between the Eden and Caldew the only evidence is the following.
In the Petterill there is a small section, showing rock like that at
Cummersdale, a few yards above the house called Petterill Bank ;
and the record of a boring at Garlands Lunatic Asylum tells us that
LIASSIC ROCKS OF THE CARLISLE BASIN. 291
below 28 feet of drift 277 feet of red stone with white bands were
pierced, which seemed to the borer to resemble “ Lazonby stone.”
Now “ Lazonby stone” is, in other words, Penrith (the great Lower
Permian) Sandstone ; but it is in the highest degree improbable that
Penrith Sandstone would be found near the surface at Garlands,
the natural presumption being that both St.-Bees and Kirklinton
Sandstones overlie it there. A very simple explanation, however,
suggests itself. The Penrith and Kirklinton Sandstones resemble
each other very much in colour, and equally differ in that respect
from the St. Bees. Both the Penrith and St.-Bees Sandstones are
largely quarried—the former about Lazonby and Penrith, the latter
near Curthwaite and Aspatria; but the soft Kirklinton stone is
scarcely ever quarried, and is well shown only in localities that are
but little generally known or visited. Hence the testimony of the
borer, though decidedly against the supposition that the stone in the
bore-hole was St. Bees, is not really against the view that it was
Kirklinton Sandstone, as I have no doubt-was the case. Its outcrop
hereabouts will keep a little east of Warwick and west of Scotby
and Carleton, abutting against the Newbiggin and Cummersdale
fault in the neighbourhood of Brisco Hall.
The Kirklinton Sandstone is nowhere visible in the sectionless
country between the Eden and Hether Burn; but in the latter
stream it may be seen from Hether-Bank Bridge to its junction with
the Line. At and above Hether-Bank Bridge are quarries in St.-
Bees Sandstone, the dip being about south-west. At Cliff Bridge,
Kirklinton, the Kirklinton Sandstone is extremely well displayed,
and it may be seen, on ascending the Line, as far up as Shield Green,
between Kirklinton Hall and the Muckle Linn. Between Shield
Green and Brackenhill Tower is St.-Bees Sandstone, and above
Brackenhill Tower Carboniferous beds (mainly sandstones and shales)
are brought in by a fault which ranges nearly north and south, and
may be seen crossing the river close to the Tower.
Between Shield Green and Kirklinton Hall a bed appears in the
Kirklinton Sandstone much resembling that of St. Bees; andin this
harder band are two quarries, one in the northern corner of Hirst
Wood, the other on the right bank of the river at Stag Ford. From
the dip, these two quarries are in all probability in the same bed,
and the St.-Bees-like stone need not be more than about 30 feet
thick.
There are no signs of faults, and the St.-Bees-like rock is evi-
dently interbedded with Kirklinton Sandstone of ordinary appear-
ance. This circumstance seems worth noting here, as, combined with
the want of any evidence of unconformity between the two formations
at Shield Green, it tends towards a totally different view from that
pointed at by all the rest of the evidence bearing on the relations of
these two beds.
Below Cliff Bridge the Kirklinton Sandstone may be seen as far
down as Metal Bridge, a little below the junction of the Esk and Line,
being well shown at Westlinton. (I have already mentioned the
boring at Justice Town, which showed 170 feet of Kirklinton Sand-
292 T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
stone above St. Bees.) Ascending the Esk it appears beneath Long-
town Bridge and at various spots in the neighbourhood of Kirk-
andrews Tower ; also about the outfall of Carwinley Burn, and up
that stream as high as Carwinley Mill. At the mill the junction
with the St. Bees is well shown. Itseems to me that there is some
slight evidence of unconformity between them at this point, West
of the Esk, Kirklinton Sandstone is seen in the lower part of the
course of the Glinger Burn, and St. Bees nearer Scots Dyke. AIL
that can be said of its western outcrop is that it must keep a little
westward of the various exposures in the Glinger Burn and at Metal
Bridge and Rockcliff, and eastward of the Gypseous Shales of Bow-
ness. It probably runs below the Lias in the neighbourhood of
ark Bampton.
It will be remembered that the Kirklinton Sandstone seen at
Cummersdale was invariably red, lke that of Kirklinton or
Netherby ; but at Holmhead, in higher beds, a borehole recorded by
Mr. EK. W. Binney* pierced through 108 feet of white sandstone,
overlying 117 feet (not through) of red. At Carlisle Gaol the bore-
hole was through 250 feet of red sandstone ; while at Messrs. Dixon
and Co.’s, West Tower Street, I was informed by Mr. John Hamil-
ton that 123 feet of white sandstone were penetrated. Other ex-
amples might be given. Lastly, in a boring at Stainton, in still
higher beds, 360 feet of white or grey stone were proved above an
unknown thickness of red. Thus the Kirklinton Sandstone appears
to consist of a lower red, a middle red and white, and an upper
white series of beds.
The Stanwix Marls probably nowhere attain any considerable
thickness. Their most characteristic colours are red and greenish
grey. They vary very much in hardness, stony bands being much
more common in some places than others. They lie between Cliff
Bridge on the north and Carlisle on the south, Houghton on the
east and Beaumont on the west. They are well shown on the Eden
in the lower part of the cliff at Etterby Scaur, from the North
British railway-bridge to Grinsdale, and about Beaumont, the sec-
tions in the two last-named localities being in the left bank of the
river. On the Line their junction with the underlying Kirklinton
Sandstone may be very plainly seen, both at Westlinton and near
Cliff Bridge. At Westlinton it appears in the bank bounding the
alluvial flat, a few yards east of the bridge. Nearer Cliff Bridge 16
is plainly shown in the little plantation bordering the alluvium,
about midway between Cliff Bridge and High Alstonby. The marls
appear here and there in the little streams that unite and fall into
the Line between Low Alstonby and Westlinton ; they are visible
nearly as far eastward as Stonystonerigg.
Before taking leave of the neighbourhood of Kirklinton, which is,
as we have seen, perhaps supreme in geological interest among the
localities mentioned in this paper, I may remark that the scenery of
the Line above Cliff Bridge is very picturesque for many miles and
very different from that below it. Both scenery and geology, how-
* Mem. Lit. & Phil. Soc. Manchester, ser. 3, vol. ii. pp. 843-388.
LIASSIC ROCKS OF THE CARLISLE BASIN. 293
ever, have hitherto been entirely ignored by writers on the geology
of North Cumberland, as well as by the authors of guide-books;
for, though Cliff Bridge itself is only about two and a half miles
from Longtown or Lyneside stations, trains stopping at those places
are few and far between, and every mile higher up the Line increases
the distance from the railway by that amount; while eastward lies
the lone bare district of Bewcastle, destitute alike of railways and
inns.
The extent of the area covered by the marls, south of the Eden,
is doubtful, but the evidence available tends to show that it is very
small. Though they form the lower part of the cliff at Etterby
Scaur, the three new railway-bridges across the Caldew, the lowest
of which is close to the junction of the North-British and Caledonian
Railways, are all founded on the underlying sandstone, the marls
not having been met with at all; and they were absent in the wells
at Messrs. Carr’s, Caldewgate, and Messrs. Dixon’s, West Tower
Street : also in that at the Gaol. On the other hand, I saw them
in an excavation at the foot of Gaol Brow, on the north side of the
Gaol, and have observed traces of them at the bottom of deep drains
in Bank Street, Lowther Street, and opposite Cavendish Place in
the Warwick Road; but their thickness hereabouts, where they
exist, must be very trifling.
West of the Caldew the evidence is much scantier. In addition
to the well at Messrs. Carr’s, already mentioned, Mr. KE. W. Binney
records (in the paper before quoted) that at the pumping-engine for
the canal by Edenside, immediately above the red and variegated
marls, there was a section in the pump-well which distinctly showed
the marls at the top gradually passing down into the red sandstone
below. Again, at Stainton, on the north side of the Eden, between
Carlisle and Grinsdale, a boring showed them to be only 23 feet
thick. In the Eden, south of Stainton, the beds are lying nearly
flat, except near the North-British railway-bridge, where north-
easterly and north-westerly dips occur. There is no evidence as to
their thickness near Beaumont.
The above facts, when combined with the great change in direc-
tion of the outcrop of the marls between Rickerby and Caldewgate,
from about N.N.K. and 8.8.W. at the former, to nearly east and
west at the latter place, seem to point to their very slight extension
below the Lias. Most of the Lias probably rests, therefore, on the
Gypseous Shales west of Great Orton, and on the Kirklinton Sand-
stone east of that village, the Stanwix Marls underlying the Lias
only in the neighbourhood of Bellevue.
Fresh borings for coal in the Lias district not being probable, the
existence of Rheetic beds is likely to remain an open question. No
evidence of them has yet been discovered, all fossils hitherto found
having been determined by Mr. Etheridge (our President) to be
Lower Lias ; but so drift- covered is the country, and so few and small
are the sections, that negative evidence must go for very little in
settling the question. The Lias country is purely agricultural, and
wells sunk for the supply of farm and other houses are usually only
Q. J.G. 8S. No. 146. x
294 T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
from 15 to 20 feet deep, or perhaps half the average thickness of the
Glacial*drift. Indeed a well-sinker, living near the southern border
of the Lias*, informed me, mistaking the motive of my inquiry,
that I need not be afraid of meeting with any rock below the drift
in the locality around his home, as he had sunk at various places he
mentioned to depths of 20, 30, or 40 feet without penetrating any
thing but sand, gravel, or clay ; for instances in which water,
attained on reaching a clayey stratum of drift, has been lost on
touching porous sandstone below, have made well-sinkers very care-
ful not to go a single foot lower than is absolutely necessary in the
case of ordinary dwellings.
The Lias area has, during the last 250 years, been much explored
in search of evidence of coal. It will not seem strange that such
has been the case, when it is remembered that the dark shale form-
ing so large a proportion of the rock visible would naturally seem
identical with the dark shale of the Coal-measures, and a striking
contrast to the red Permian and Triassic beds around. The non-
Carboniferous, and probably Liassic, nature of the formation was
first discovered by Mr. R. B. Brockbanky, who, on finding Ammo-
nites and other fossils in Thornby Brook, sent them to Mr. E. W.
Binney, who pronounced them to be Liassic. Mr. Binney after-
wards visited the district and recorded the result in a paper read
before this Societyt. JI have since discovered but one section not
described therein, in a brook between Great Orton and Flat. It is
composed of dark shale with limestone bands. Ammonites John-
stont was found there, as also in Thornby Brook and at Quarry Gill,
near Aikton. By Mr. R. B. Brockbank’s assistance I was enabled
to obtain evidence of the thickness attained by the lias between
Great Orton and Flat, a spot nearly at its centre. A document, from
which J have already quoted, which has been preserved by the Stordy
family of Great Orton, gives the following details, according to a
copy of it kindly made for me by Mrs. Hannah Pearson, of Station
Hill, Wigton. In the year 1781 a boring was made by John Brisco,
of Crofton, in John Stordy’s Gill close. A blue stone was found
18 feet from the surface, and ‘different stone, mostly bluish,” till
they arrived at a depth of 228 feet. Then they pierced the “red
stone or clay, sometimes mixed with veins of white” (which I sup-
pose to be the Gypseous Shales), till they came to a depth of
360 feet.
The Lias area forms a plateau, with a slightly greater general
elevation than is attained immediately outside it. This plateau-like
character is better marked in the country between Aikton and Great —
Orton than eastward of the latter place. No person standing about
Wiggonby, near the southern border of the Lias, can fail to notice the
difference between the flat-topped plateau northward and the rolling
drift-ridges to the south. But though this change of feature makes
it possible to map the Lias boundaries with some approach to a
_* Andrew Miller, Nealhouse.
+ Of Moor Park, Crosby, near Maryport.
+ Quart. Journ. Geol. Soc. vol. xv. p. 549.
LIASSIC ROCKS OF THE CARLISLE BASIN. 295
fairly good general line, the persistently drift-covered surface
prevents any ‘thing like precision.
In conclusion, ‘T will briefly pass in review the leading points
bearing on the relations of the beds described to each other, which
are illustrated in the diagram sections (figs. 1-3, p. 296).
The St.-Bees Sandstone has been shown to surround the overlying
beds, its general dip varying from north to a few degrees north of
west, between Maryport and the Eden. In the Hether Burn, Line,
and Carwinley Burn its general dip is more or less south of west ;
and west of the Esk it varies between south-east and south. There
can be no doubt that the St.-Bees Sandstone is the lowest bed of a
true basin, the western limits of which are now below the Solway.
Then, first of the overlying beds come the Gypseous Shales, which,
strange to say, are nowhere exposed to view, but are known on the
evidence of the boreholes at Abbey Town and Bowness, and, perhaps
I may add, that at Great Orton. Their invisibility is mainly caused
by the special thickness and persistence of the drift over the ground
they occupy, but also, at Cummersdale, to the probable interposi-
tion of a great fault. There is no evidence of any kind suggesting
unconformity between the Gypseous Shales and the St.-Bees Sand-
stone; and, on the other hand, as Gypseous Shales underlie the
St.-Bees Sandstone near Carlisle, gypsum is evidently hereabouts a
Permian characteristic. I have accordingly classed the Gypseous
Shales as Permian.
The Kirklinton Sandstone, however, appears to rest unconform-
ably on the Gypseous Shales to the west, and on St.-Bees Sandstone
to the east and north-east of Carlisle. But not only do the Gypseous
Shales disappear towards the north-east, but the greater part of the
St.-Bees Sandstone is also missing. Six or seven miles south-east
of Carlisle the thickness of the St.-Bees Sandstone is estimated by
Mr. J. G. Goodchild at from 1500 to 2000 feet; but in the Hether
Burn there can hardly be more than 800 feet of Permian rock, from
the breccia at its base to the outcrop of the Kirklinton stone below
Hether-Bank Bridge ; and in Carwinley Burn, between the breccia
at the base of the Permian formation and the outcrop of Kirklinton
stone at Carwinley Mill, there cannot be more than 250 feet of rock.
In both these burns there is an almost continuous series of sections,
and there are no signs of faults. Both about Brampton on the one
hand and west of the Esk on the other the thickness of the St.- Bees
Sandstone must be very much greater. Two outliers of Kirklinton
Sandstone exist—one at Canobie, opposite the church, resting on
Carboniferous rock; the other on the Cambeck near Walton, resting
on St.-Bees Sandstone. ‘Thus the band of St. Bees-like rock seen in
_ the Kirklinton Sandstone on the Line goes for nothing when the
whole of the evidence is considered, important as it would be did it
stand alone. In poupcamence of this decided unconformity to the
beds below, I have classed the Kirklinton Sandstone as Bunter.
- Itis evident that the Stanwix Marls, in their turn, repose uncon-
_ formably on the Kirklinton sandstone ; for while at Cliff Bridge and
_ Westlinton they rest upon the lower red beds, at Stainton and
Kee
T. V. HOLMES ON THE PERMIAN, TRIASSIC, AND
296
“Sel ‘3 ‘S[Te], XIMULIQ “p
“Tne
p22 Q* oo Do Ton Bower?
af DEO ES Pate tl Rel L sire
Or aha 0 67 ous SSS eS
> SS ———__——— =, as
° a em =
I
|
“OUITeM 99D TAL
ooduie AA TAA
-uopbr yy fo ymnos yung oy) 07 ‘a.nyssrufung “quog flopsoy, mors uoyooy oynuunuhrrg—¢ “OL
“098,
‘uoyd meg
TN
"wopduDrg au
0,”
‘£qus0yy,
———— =——
“uOPATY JO
4seo o[IU @ ITU
I Ae) CIE nie
Sa ——
seer h
a Ver “4s boa
UOFLO TIT
UOP ET
a
“TOIsery
oAly
= “kemjog "‘qUIOg FOpPAOT,
“N
064° 80g
eo Che es DOs omnes
! SG 820 % Foy
2 I | ———
\ P
1
i)
“ISH TOA ‘sso Avmjog “KT
“uopsyng 07 ssopy hnmpoy mouf uoyragy synununebhnig—% “Suit
*XIMUvYG
0}
MOJIO YCOTD
‘umoy, Aoqqy “VMOU
‘fiquopp fo yrwou ‘imampoy 4) worl wojooy synuunihmrg— | “oli
LIASSIC ROCKS OF THE CARLISLE BASIN, 297
Grinsdale they le upon the upper white ones. In consequence of
this decided unconformity the Stanwix Marls are here classed as
Keuper.
And there seems to me to be little doubt that the Lias, in its turn,
rests unconformably on formations all of which are unconformable
to each other—the Gypseous Shales, the Kirklinton Sandstone, and
the Stanwix Marls. But as in this case it is barely possible, though
not, I think, probable, that the Stanwix Marls may overlap the two
lower formations and underlie the Lias throughout its area, the
possibility seems worth mentioning.
In this paper such facts only have been brought forward as
seemed necessary to establish the true relations of the various for-
mations to each other, fuller details being reserved for a forthcoming
memoir.
Nore on the Lias. April 25, 1881.
Since writing my paper, my attention was called by my friend
Mr. H. B. Woodward to a passage in a paper by Rev. J. E. Cross
*‘On the Geology of North-west Lincolnshire ” (Quart. Journ. Geol.
Soc. vol. xxxi. p. 116). Mr. Cross remarks that in the neighbourhood
of Appleby he has not been able to detect any Rheetic fossils, though
he has searched diligently for them. He says, “ the first strata
next above the Keuper are those which contain Ammonites angulatus
and A. Johnston.” He also remarks that A. angulatus has the
ereater range, and extends throughout a zone of 150 feet or
more.
In Cumberland A. Johnstont must have a range fully equal to that
of A. angulatus in North-west Lincolnshire.
In a letter received from Mr. Cross, dated February 22nd, 1881,
he states that he has not since detected any Rheetic fossils in the
above-mentioned locality, but that, as they may be seen both near
Gainsborough on the south and across the Humber on the north, it
is very possible that they nevertheless exist there. He also remarks
that as “‘A. angulatus is one of the most persistent of Ammonites in
its own place, and A. Johnstoni, whenever it appears, ranges from
the middle of the A.-angulatus-beds to strata below those in which
A. angulatus is ever seen, I think if you find A. Johnstoni and do
not find A. angulatus, you must be below the A.-angulatus-beds
altogether.”
Prof. J. W. Judd, in his paper on ‘“‘ The Secondary Rocks of Scot-
land” (Quart. Journ. Geol. Soc. vol. xxxiv. p. 697); remarks that the
zone of Avicula contorta does not appear to be distinctly developed
in the West Highlands, while the Infralias (Planorbis- and Angulatus-
zones) attains a thickness of from 150 to 200 feet.
EXPLANATION OF PLATE XI.
Sketch Map showing the rocks of the Carlisle basin: scale 4 miles to | inch.
298 ON THE PERMIAN ETC. ROCKS OF THE CARLISLE BASIN.
Discussron.
Mr. Baverman, having experienced the extreme difficulty of
understanding the rocks of this district from the obscurity of the
evidence, bore testimony to the great care and skill with which
the author had worked out such an unpromising subject.
Prof. Jupp remarked upon the great interest attachiug to the
outlying patch of Lias near Carlisle. The author had now, for the
first time, made us acquainted with the thickness of these Lias
strata, and proved that it exceeded 200 feet. So far as the evidence
went, they belong entirely to the Infralias, and the same member
of the Lias was also abnormally thick on the west coast of Scotland.
The numerous unconformities pointed out by the author as existing
among the red rocks below seemed to show that but little value
should be attached to such local unconformities in classifying the
strata.
Mr. Wartaker said that his colleague Mr. H. B. Woodward pro-
posed to group the whole of these red rocks under the comprehensive
term Poikilitic, and thought that the Rheetic beds are most likely
present in the area, although not seen. He spoke of the unsafe
character of the colour-test in classifying rocks.
Rev. J. F. Buaxs asked as to the evidence of the existence of as
much as 200 feet of Lias beds belonging entirely to the lowest part
of the series, and as to the proofs of the existence of an uncon-
formity between the Stanwix Marls and the Lias.
Prof. T. Rurrrr Jones protested, with reference to the use of the
word ‘ Poikilitic,” used by preceding speakers indicative of anti-
Permian views, that there had been good grounds for John Phillips
and others to determine and establish the Permian Series, and that
there were no good grounds for its being again amalgamated with
the overlying series.
The PRESIDENT said that no evidence of the occurrence of Rheetic
fossils in the area had ever been found, but that possibly the
Stanwix Marls might have to be classed with the Rhetie Tea-
green Marls of the Bristol area. The Lias of Adderley was let down
by means of great faults below the ievel of the Keuper marls.
The Avrnor said that he advanced his classification as a purely
provisional one. He did not think it probable, though it is barely
possible, that the Stanwix Marls underlie the Lias. In classing
certain of these beds as Permian, Bunter, or Keuper, the author
chiefly desired to mark their relative positions and affinities, the
latter being determined by the existence or non-existence of un-
conformities between them.
Quart. Journ .Geol.Soc Wolke
SG; ae Cc
» OCH. NEES
OPO Pee) bt aii ON OoNG 9 Bt SRO =
ete
~ SDRAG lS 205 BLO Se
Ns aR ¥
eh Mh our aire iG
% pepe Mtl ee int 14:2
io hell a0 3 SR
iN il it~ Sgt
ies ee Ae i
alc (ex erie dl
A.S.Foord del Mintern Bros 1p.
DEVONIAN PLANTS.
Quart. Journ. Geol .5oc Vol OOWiiee eae
A.S.Foord del. Mintern Bros. mp.
DEVONIAN PLANTS.
ON NEW ERIAN (DEVONIAN) PLANTS. 299
23. Nores on New Ertan (Devontan) Prants. By J. W. Dawsoy,
LL.D., F.R.S., F.G.S., Principal of M°Gill College, Montreal.
(Read June 23, 1880.)
[Prares XII. & XIIL]
THE principal purpose of the present paper is to add a few new facts
to our knowledge of the Precarboniferous flora of Eastern America.
Since the publication, in the Journal of this Society, of my paper,
“Further Observations on the Devonian Plants of Maine, Gaspé,
and New York” (1863), and that on “Fossil Ferns of the Devo-
nian ” (1871), a large addition was made to the knowledge both of
the species of plants and of the general character and conditions of
Devonian and Upper Silurian vegetation in my “Report on the
Devonian and Upper Silurian Plants of Canada”*. In a subsequent
report on the “ Plants of the Lower Carboniferous and Millstone
Grit”7, I endeavoured, by the aid of the American formations, to
remove the perplexities that had been caused by the disputes re-
specting the age of the Kiltorcan beds in Ireland and the so-called
“‘Ursa-stage ” of Bear Island, difficulties which, however, still appear
to constitute subjects of discussion.
In 1878 I contributed a paper to the Geological Society of Edin-
burgh, entitled ‘‘ Notes on Scottish Devonian Plants,” comparing
these plants with those of America, and at the same time establish-
ing the genus Péilophytont for those remarkable pinnately-leaved
Lycopodiaceous plants of which Lycopodites Vanuxemu of the De-
vonian of New York and LZ. plumula of the Lower Carboniferous of
Nova Scotia are types, and of which Pt. Thomsoni is a Scottish re-
presentative described in the paper above referred to.
Since the publication of these reports and papers several interest-
ing new forms have come into my hands from the Devonian or Erian
of North America, to which I shall add two new species, one from
Scotland and one from Australia, kindly communicated to me by
friends in those countries.
Plants from the Erian (Devonian) of New York.
1. AsTHROPTERIS NOVEBORACENSIS, gen. & sp.n. (Pl. XII. figs. 1-9.)
The genus Asteropteris is established for stems of Ferns having the
axial portion composed of vertical radiating plates of scalariform
tissue imbedded in parenchyma, and having the outer cylinder com-
posed of elongated cells traversed by leaf-bundles of the type of
those of Zygopteris.
* Geol. Survey of Canada, 1871, pp. 100, 20 plates.
+ Ibid. 1873, pp. 47, 10 plates.
{ Ptilophyton may perhaps he considered too near to Psilophyton, but the
sound of the names is quite different. In a recent Report of the Regents of
New York, Hall has stated his belief that Pt. Vanuxemii is not a plant but a
zoophyte. He does not fully state the reasons for this conclusion ; but should
this view be established with regard to this species, then Géppert’s Lycopodites
penmneformis or my L. plumula may serve as the type of the genus.
300 DR. J. W. DAWSON ON NEW
The only species known to me is represented by a stem 2°5 cen-
timetres in diameter, slightly wrinkled and pitted externally, per-
haps by traces of aerial roots which have perished. The transverse
section shows in the centre four vertical plates of scalariform or
imperfectly reticulated tissue, placed at right angles to each other,
and united in the middle of the stem (figs. 1-4). At a short distance
from the centre, each of these plates divides into two or three, so as to
form an axis of from ten to twelve radiating plates, with remains of
cellular tissue filling the angular interspaces (fig. 3,6). The greatest
diameter of this axis is about 1°5 centimetre. Exterior to the axis
the stem consists of elongated cells (fig. 7), with somewhat thick
walls, and more dense towards the circumference. The walls of these
cells present a curious reticulated appearance, apparently caused by
the cracking of the ligneous lining in consequence of contraction in
the process of carbonization. Imbedded in this outer cylinder are
about twelve vascular bundles (figs. 2, 3,d@), each with a dumb-bell-
shaped bundle of scalariform vessels enclosed in a sheath of thick-
walled fibres. Hach bundle is opposite to one of the rays of the
central axis. The specimen shows about two inches of the length of
the stem, and is somewhat bent, apparently by pressure, at one end.
This stem is evidently that of a small tree-fern of a type, so far
as known to me, not heretofore described *, and constituting a very
complex and symmetrical form of the group of Paleozoic Ferns
allied to the genus Zygopteris of Schimper. The central axis
alone has a curious resemblance to the peculiar stem described by
Unger (‘ Devonian Flora of Thuringia’) under the name of Cladoaylon
nurabile; and it is just possible that this latter stem may be the axis
of some allied plant. The large aerial roots of some modern tree-
ferns of the genus Angiopteris have, however, an analogous radiating
structure.
The specimen is from the collection of Berlin H. Wright, Esq.,
of Penn Yan, New York, and was found in the Portage group
(Upper Erian) of Milo, New York, where it was associated with
large petioles of ferns and trunks of Lepidodendra, probably L.
chemungense and L. primavum.
In previous communications to the Society I have described three
species of tree-ferns from the Upper and Lower Devonian of New
York and Ohio; and this species is from an intermediate horizon.
All four occur in marine beds, and were, no doubt, drift-trunks from
the fern-clad islands of the Devonian sea. The occurrence of these
stems in marine beds has recently been illustrated by the observa-
tion of Prof. A. Agassiz, that considerable quantities of vegetable
matter can be dredged from great depths in the sea on the leeward
side of the Caribbean Islands. The occurrence of these trunks
further connects itself with the great abundance of large petioles
(Rhachiopteris) in the same beds, while the rarity of well-preserved
fronds is explained by the coarseness of the beds and also by the
probably long maceration of the plant-remains in the sea-water.
* Prof. Williamson, to whom IJ have sent a tracing of the structure, agrees
with me that it is new.
ERIAN (DEVONIAN) PLANTS. 301
2. Eauisutipes WrigHTIANA,sp.n. (Pl. XII. fig. 10& Pl. XIII. fig. 20.)
This is a specimen in the same collection with the above. It is
a cast in sandstone, 6 centimetres in diameter, with nodes from 4 to 5
centimetres apart. The surface has a slight carbonaceous coating
and is finely tuberculated, the tubercles being very regularly
arranged, and representing the bases of very short hairs or bristles,
which are seen entering the surrounding matrix. Impressions
above the joints appear to indicate sheaths, each of about twelve
broad leaves, which are abruptly narrowed and acuminate at the top,
and show an indication of a median nerve or rib (fig. 10). The leaves
of the sheaths are 1 centimetre broad and 1°7 centimetre long. It
would be possible, however, to interpret these supposed sheaths as
due to mere plications or foldings of the epidermis; and in this case
the plant may have borne verticils of leaves, of which these sup-
posed sheaths may be merely the remains. ‘The first explanation,
however, appears more probable; and, if it is correct, the plant is a
- true Hgwisetides, and the present specimen is the first occurrence of
this genus in beds older than the Carboniferous. It is to be observed,
however, that ‘Unger has described from the Cypridina-slates of
Thuringia plants of the genera Kalymma and Asterophyllites (A.
coronata) with sheaths at the nodes; and my A. scutigera, from St.
John’s, has verticils of scales at the joints, which may represent
sheaths. The present species has a remarkable resemblance in its
markings and the form of its sheaths to a greatly magnified stem of
the modern Hquisetum fluviatile, except that the leaves of the sheaths
are shorter.
The species is named in honour of its discoverer. Its essential
characters will be as follows :— 3
Stem stout, cylindrical or broadly ribbed, surface marked with
short hairs or tubercles regularly arranged. Sheaths at the joints,
of about twelve leaves, of the general form of those of Hquisetuimn
fiiatile.
The specimen is from the Portage group (Upper Erian) of Italy,
New York.
3. CYCLOSTIGMA AFFINE, sp.n. (Pl. XII. figs. 11 & 12.)
Stem marked with alternate circular leaf-bases or areoles, slightly
prominent below, evanescent above, and each with a circular dot or
vascular mark. Scars scarcely two millimetres in diameter, and
separated by finely corrugated bark, about twice their diameter
apart. These markings occur on a stem about an inch in diameter.
The Knorria, or decorticated form of this plant, presents irregular
waving ridges, produced by the longitudinal confluence of the oblique
vascular bundles.
This plant is the nearest approach to the well-known C. kiltorkense
of Ireland hitherto found in America. It differs chiefly in the more
closely placed areoles. It was collected by Mr. Wright, and is from
the Chemung (Upper Erian) of Italy, New York. The study of this
plant has led me to the belief that Stigmaria ewiqgua of my Report
of 1871 may, when better known, prove to be a new species, allied
to the present, and a member of the genus Cyclostigma.
302 DR. J. W. DAWSON ON NEW
4, LEPIDODENDRON PRIMzVUM, Rogers. (PI. XII. fig. 13.)
Mr. Wright’s collection contains fragments of a Leprdodendron
from Milo, New York, which seems to belong to the species above
named, but presents the curious peculiarity of having the leaf-bases
depressed instead of being prominent. This may result either from
some peculiarity of pressure or from the leaf-bases being deciduous
and leaving depressed scars when removed. In either case these
specimens illustrate this peculiarity as seen in the Lower Silurian
Glyptodendron of Claypole, which may possibly have had decorti-
cated leaf-bases. Specimens of this kind, of course, retain no distinct
vascular marks, and the impression on the matrix resembles those
decorticated Lepidodendra of the Coal-formation which used to be
named Lyginodendron, but which, in Nova Scotia at least, usually
belong to the species Lepidodendron rimosum,
5. CELLULOXYLON PRIMMVUM, gen. & sp. n.
A silicified trunk, showing in cross section large and somewhat
unequal hexagonal cells, with an appearance of Knes of growth
caused by concentric bands of smaller cells. No medullary rays.
The longitudinal section shows either cells superimposed in vertical
rows, or a sort of banded prosenchymatous tissue; but the structure
is much masked by the crystallization of the quartz.
This specimen is from the collection of Prof. J. M. Clarke, of Am-
herst, Massachusetts, and was obtained from the Hamilton (Middle
Erian) of Canandargua, New York. It was undoubtedly a woody
stem and not an Alga; but its structure is even less specialized than
that of Prototaxites, from which it differs in the want of medullary
rays, and in its less distinctly elongated wood-cells without spiral
markings. It has some resemblance to Aphyllum paradoaum of
Unger, but is more uniform in its structure. It adds another to
those mysterious woody stems of doubtful affinities which, in the
Devonian or Erian of both sides of the Atlantic, represent the
Taxinez and Conifers of later formations.
Additional specimens received from Prof. Clarke show that the
appearance of rings of growth is caused by large cells disposed in
concentric narrow bands between the wider bands of fine fibrous
tissue. In the longitudinal section these bands of large cells appear
to be parenchymatous and not vascular. There are no medullary
rays, but rounded patches of cellular tissue appear here and there
in the fibrous layers. The structure is thus very peculiar, and ap-
pears to have been the result of a kind of exogenous growth, in which
coarse parenchymatous layers were deposited between the periodical
rings of the stem, reminding one of the bark-like layers interposed
between the growth-rings in G'netwm and in some tropical climbers.
The stem of the present plant was, however, in all probability, of
much more simple character, though woody and capable of resisting
pressure. It is to be observed also that the specimens neither show
the structure of the pith or bark, and that the finer structures of
the tissues preserved must have been partially obliterated by the
ERIAN (DEVONIAN) PLANTS. 303
eranular crystallization of the quartz with which the specimen is
mineralized.
Miscellaneous Specimens from New York.
Numerous large petioles of Ferns occur in collections sent to me
by Mr. Wright and Dr. Parker of Ithaca, New York. Being desti-
tute of the fronds, it seems unnecessary to describe them more
particularly ; but they indicate the possibility that the Erian of New
York may yet afford a rich Fern-flora comparable with that of St.
John, New Brunswick. In collections made by Mr. Wright are
also specimens of those singular plants, supposed to be Alge,
which Hall has named Dictyophyton. A very fine specimen of one
of the species was figured in my paper of 1863, under the name
Uphantena chemungensis, originally bestowed on one of the species
by Vanuxem, but which is rejected by Hall in favour of the generic
name above given. The specimens sent by Mr. Wright do not give
any additional information as to the mode of growth of these curious
forms; but he has found in the Hamilton formation, not previously
known to contain these plants, a species probably distinct from
those described by Hall, and which may be named D. hamiltonense ;
though if these plants were really Alge, the supposed species
may be nothing more than varietal forms or stages of growth.
The specimens referred to are unequally turbinate or unequally
conical in form, rapidly expanding from the base, and marked with
sharp longitudinal ridges, crossed with much finer and more
frequent revolving lines. The largest specimen is almost 13 inch in
diameter, narrowing to less than 1 inch in a length of less than
2 inches.
The remarkable spiral plant belonging to the genus Spirophyton
of Hall, the “* Cauda-galli fucoid” of the earlier Reports on the State
of New York, is found in the same beds with Dictyophyton. It is
also found, as mentioned in my paper of 1863, in Gaspé, where it
ranges from the Upper Silurian into the Lower Devonian. Plants
of the same genus have been found by the late Prof. Hartt on the
Rio Tapajos, in Brazil, in beds referred to the Carboniferous period,
though some other plants found in the same beds might in North
America be supposed to be Upper Devonian in age. In MS. descrip-
tions of these plants sent to Prof. Hartt, and which may have been
published in his Reports, I named this species S. brasiliense. It is
of interest as showing the very wide distribution of this form in the
paleeozoic seas.
Plants from the Erian (Devonian) of St. John, New Brunswick.
I have recently obtained, from the widow of the late lamented
Prof. Hartt, the remainder of his Devonian plant-collections, con-
sisting principally of duplicates of the more common species found
at St. John, but with a few fragments indicating forms not pre-
yiously known to me.
Since the publication of my papers and reports on the fossils of
the St.-John beds, they have been repeatedly referred to by Kuropean
304 DR. J. W. DAWSON ON NEW
palzobotanists as Lower Carboniferous, apparently on no better
grounds than their superior richness in plants to the Devonian of
Europe. On this account it may be desirable here to summarize
the evidence now available as to their actual age. This may be
stated thus:—(1) The Dadoxylon Sandstone and Cordaite shale
of Southern New Brunswick are folded up and partially altered with
the Silurian and Cambrian rocks of the district, and are overlain
unconformably by the Lower Carboniferous conglomerates (Subcar-
boniferous of some American geologists). These conglomerates are,
further eastward, associated with beds holding the characteristic
fossil plants of my Horton series, equivalent to the Tuedian or
Calciferous series of Scotland. There is also evidence that the
Devonian plant-beds are anterior to the great intrusive Devonian
granite of this region, whose débris are found in the Lower Carbo-
niferous conglomerates, but not in the underlying rocks. ' Additional
facts illustrative of these points will be found in the Reports of
Messrs. Bailey and Matthew in the publications of the Geological
Survey of Canada for 1871 and 1875.
(2) The flora of these beds is markedly different from that of the
Lower Carboniferous, of the Millstone Grit, and of the true Coal-
formation in New Brunswick and Nova Scotia, all of which have
been studied and described.
(3) The prevalent forms in the St.-John beds are those character-
istic of the Devonian in Gaspé, New York, and Maine, such as Arche-
opteris, Cyclopteris obtusa, Psilophyton, Calamites radiatus, Dadoxylon
ouangondianwm, though several genera are common to these beds and
the Carboniferous. The fact that the flora of these beds is richer
than that of the Huropean Devonian, and contains types which
appear later in Kurope, is in harmony with known facts as to the
earlier appearance of plants in America in other stages of geological
history. JI may add that some of the genera noticed in 1863 from
St. John, and not then known in the Devonian of Europe, have sub-
sequently been found there. ven as late as 1879 some of them
were discovered by Peach in the Old Red of Scotland.
(4) The new facts which have been disclosed, more especially those
which indicate the great richness of the Devonian flora of New York
in Ferns, now induce me to believe that these St.-John beds, though
rivalling the Coal-formation in their abundance of fossil plants, are
really of the age of the Hamilton group of New York, which in
Europe would be regarded as Middle Devonian.
(5) I would further add that the richness of this flora in species,
as well as the discovery of rare and exceptional forms, such as insects,
is in part due to the excellent exposure of the beds in the vicinity of
St. John, and in part to the extensive and thorough nature of the
explorations carried on with the aid of blasting by Messrs. Hartt
and Matthew, under the auspices of the Natural-History Society of
New Brunswick. It is probable that few fossiliferous beds in the
world have been so thoroughly explored. In connexion with this
it is to be observed that the mass of the specimens obtained repre-
sents only a few species, while the greater number are represented
ERIAN (DEVONIAN) PLANTS. 305
by only a few fragments, which would undoubtedly have escaped
the observation of ordinary collectors.
In the collections now in my hands the following forms occur,
which may be considered new, though most of them are too imper-
fect for complete description.
ODONTOPTERIS sQuaMOSA, sp. n. (Pl. XIII. fig. 17.)
Petiole slender, bearing short pinnules placed at right angles to it,
and each consisting of two rounded decurrent pinnule and a terminal
pinnule of triangular form. Toward the end only the terminal
pinnule appears. Veins obscure, diverging from a midrib, broad at
base. Frond apparently of a thick or coriaceous texture.
This would seem to have been a creeping or parasitic Fern. In its
general habit it bears some resemblance to Cyclopteris dissecta of
Unger, from the Devonian of Thuringia, but appears to have more
affinity with the genus Odontopteris than with Cyclopteris.
CARDIOPTERIS ERIANA, sp.n. (Pl. XIII. fig. 18.)
Pinnules nearly round or slightly oblong, nearly equally cordate
at base, somewhat crowded on a slender petiole. Length from 8 to
14 millim. Veins regularly spreading from the centre of the base,
curving toward the margin, and forking twice or thrice.
This is the first appearance of this Lower Carboniferous genus in
the Devonian. The species closely resembles Cyclopteris polymorpha
of Goppert, though every way smaller and more delicate.
Arc moprEris erspaae uel exunil fet al9).,)
Petiole apparently woody, bearing broadly obovate decurrent
pinnules, with strong, flabellate, straightish nerves. Pinnules over-
lapping each other.
This plant bears a general resemblance to Archwopteris of the type
of A. (Cyclopteris) Maccoyana of Goppert ; but the woody petiole
or branchlet, and the coarse texture of the pinnules, raise the sus-
picion that the specimen may not be a Fern, but may have belonged
to a coniferous tree of the type of Voltzia or Salisburya.
CYCLOPTERIS, sp.
Fragments of a very large cyclopterid leaf, with flabellate veins,
and which, when entire, must have been three inches in diameter.
It is too imperfect for description, but indicates a frond of the
Same general character with Cyclopteris Brownw from Peny, in
Maine.
Other specimens indicate a small species of Archwopteris, more
delicate than A. Jacksoni; and there are some fragments which
seem to show, though not indisputably, that the submerged leaves of
Asterophyllites latifolia were long and linear, approaching in form
to those previously described as A. lenta. A fragment of Hymeno-
phyllites, about the size and form of H. Gersdorffix, shows minute
rounded spore-cases comparable with those of the modern genus
Todea, which the Fern itself also closely resembles.
306 DR. J. W. DAWSON ON NEW
The species above described add to the number of small and
delicate Ferns by which the St.-John beds are so especially charac-
terized.
Specimens from Scotland and Australia.
/XTHEOTESTA DEVONICA, sp.n. (PI. XII. figs. 14, 144.)
Fruit 4 millim. in diameter, oval in cross section. Testa less
than 1 millim. in thickness, and consisting of radiating fibres.
Nucleus represented by white mineral matter with coaly specks.
The specimen shows only a cross section ; but there seems no reason
to doubt that it is the seed of the above genus of C. Brongniart*,
hitherto found only in the Coal-formation of France. It may be
referred to Taxinee, and may have been the seed of trees of the
genus Dadowxylon.
The specimen is in grey sandstone, associated with fragments of
carbonized plants. It was collected by the Rev. Thomas Bodun, of
Edinburgh, in the Old Red Sandstone of Perthshire, where it is asso-
ciated with Lycopodites Millert and Psilophyta.
DICRANOPHYLLUM AUSTRALICUM, sp. n. (Pl. XIII. figs. 15 & 16.)
Stem slender, 3 millim. in diameter, not tapering in a length of
3 inches. It is marked with minute, narrow, elongated leaf-bases,
spirally arranged. Leaves linear, 3 millim. long, bifurcating at an
obtuse angle at their extremities.
The specimen is in white sandstone and is well preserved. It
was collected by Mr. R. L. Jack, F.G.S., of the Geological Survey of
Queensland, in sandstones associated with limestone, on Fanning
River, Burdekin, Queensland. The horizon is said to be under the
Mt.-Wyatt and Star beds, and consequently lower than that of the
plants collected by Mr. Daintree, and described by Mr. Carruthers
in the Journal of this Society.
The genus Dicranophyllum was established by Grand’ Eury* for
certain plants of the French Coal-fields, which, though larger and
better-developed than the present species, must have been some-
what similar. Grand’Hury regards these plants as probably
Coniferous.
The plants described in this paper are fragmentary and imperfect,
but they add six or seven types to the Hrian flora, and encourage ©
the hope that all the Carboniferous genera may yet be recognized in
the older formation, together with others peculiar to itself, thus
tending to vindicate the opinion expressed in a former paper that
the plant-life of the Devonian was more varied or less monotonous
than that of the Coal-formation.
Supplementary Note.
As some delay has occurred in the publication of the above paper,
I may be permitted to add the following :—
(1) In my paper on Devonian Tree-ferns in the ‘ Quarterly
* Annales des Sciences Naturelles, vol. xx. t Flore Carbonifére.
\
—
ERIAN (DEVONIAN) PLANTS. 307
Journal’ of this Society for 1871, I referred, under the names of
Psaronius textilis and Caulopteris Lockwoodi, to certain remarkable
trunks of Ferns from the Chemung formation (Upper Devonian) of
Gilboa, New York, placed in my hands by Prof. Hall and Mr. Lock-
wood, and which were stated to be from a locality where numerous
erect trees exist. Prot. Hall has since extracted several of the
largest of these trees, and they are now in the State Geological Col-
lection at Albany, where I lately had the pleasure of examining them.
They entirely confirm my conclusions as to their nature, derived
from the fragments submitted to me, being evidently trunks of large
tree-ferns surrounded by masses of aerial roots, in some cases 2 feet
in diameter at the base, and apparently passing downward into a
shaly bed or underclay filled with rootlets. Prof. Hall hopes shortly
to publish illustrations of these remarkable trunks, representing the
oldest fossil forest yet known.
(2) In the course of last summer, the researches of Messrs. Ellis,
Foord, and Weston, of the Geological Survey of Canada, have dis-
closed, near the head of the Bay de Chaleurs, some interesting
exposures of Devonian beds rising from beneath the Lower Carboni-
ferous (Bonaventure formation of Logan). In some of these beds,
probably Middle Erian, there are abundant remains of Psilophyton,
similar to those of Gaspé Bay; but others, which are evidently
upper members of the Hrian system, contain fossil fishes referred by
Mr. Whiteaves to the genera Pterichthys, Tristichopterus, Phanero-
pleuron, and Cheirolepis. In the same beds with these fishes occur
fronds of three species of Ferns, of which I have myself collected
specimens in a visit to the locality in July last, though the best
examples have been found by Mr. Foord. One of the species is an
Archeopteris, allied to A. hibernica and A. Jackson, but differing
in the details of the fructification, which 1s well preserved (A. magna-
censis*, MS.). Another is amagnificent fern, referable in the mean-
time to the provisional genus Cyclopteris, and identical with that
figured by Lesquereux in the Report of the Geological Survey of
Pennsylvania (new series) as Archcopteris obtusa. Lesquereux’s
specimen is from the Chemung or Catskill of Montrose, Pennsylvania.
A third species is that described by me, in Quart. Journ. Geol. Soc.
vols. xviii. & xix., as Cyclopteris Brounw. In the specimens from
Bay de Chaleurs the large flabellate fronds of this fern are seen to
be attached in dense groups to a rhizome or slender stem, showing
that this plant was either, as I supposed in regard to the specimens
which I described from Peny, in Maine, a low-growing ground-fern
or an epiphyte.
(3) In the “ discussion ” of my paper I observe a statement to the
effect that Asteropteris noveboracensis may be a lycopodiaceous plant.
In reply, I think it sufficient to refer to the description and figure,
but may add that I have had occasion in previous papers to refer to
the remarkable abundance and variety of ferns in the islands of the
Devonian sea.. In accordance with this, the beds near Milo, New
York, in which Asteropteris occurs, abound in stipes of large ferns,
* Cape Magnach is the locality.
308 ON NEW ERAN (DEVONIAN) PLANTS,
while the only lycopodiaceous plant which they have afforded is
Lepidodendron primevum.
DESCRIPTION OF THE PLATES.
Puate XII.
Figs. 1, la. Asteropteris noveboracensis, cross section, natural size and enlarged.
2. A. noveboracensis, portion enlarged, showing one vascular bundle.
3. , portion enlarged 12 times, showing rays and vascular bundle.
4, —— , stem restored-in cross section.
5,6. —— , scalariform vessels, X 100.
io == , prosenchyma of outer cylinder, x 40.
8, 9. ——- ——, parenchyma of inner cylinder, x 40.
In the above figures, a represents radii of axis, 6 cellular tissue
of axis, ¢ outer prosenchyma, d leaf-bundles.
10. Equisetides Wrightiana, leaf of sheath.
ll. Cyelostigma affine.
, leaf-base, enlarged.
13. Lepidodendron primevum.
14. Aitheotesta devonica, natural size and enlarged,
Prats XIII.
15. Dicranophyllum australicum.
, enlarged.
. Odontopteris squamosa.
18. Cardiopteris eriana.
19. Archeopteris, sp. n.
20. Equisetides Wrightiana.
Discussion.
Mr. Carrutuers spoke very highly of the industry of Dr. Dawson
in collecting fossils, but he could not agree with him in his con-
clusions as to their systematic relations. He thought the form
described as a fern should be referred to the Lepidodendroids.
ON FOSSIL CHILOSTOMATOUS BRYOZOA FROM AUSTRALIA. 309
4
24, On Fossit Cuttosromatous Bryoz0a from SoutH-west Victoria,
AvstRatia. By Arraur W. Warers, lsq., F.G.8S. (Read
April 25, 1881.)
[Puates XIV.-XVIII.]
Parr of the material forming the subject of the present communica-
tion I received in exchange from Miss E. C. Jelly, in a small test-
tube, already washed out of the clay; and on two subsequent
occasions she has kindly lent me a number of slides from her col-
lection. The “lump of clay ” out of which they were washed was
sent over to England marked ‘‘ Yarra-Yarra, Victoria,’ by Mr. John
Allen some years ago; but the exact locality Miss Jelly has been
unable to obtain for me. However, I find that Mr. H. Watts, in a
paper “ On fossil Polyzoa” (in the Trans. Roy. Soc. Vict. vi. 1865,
p. 82-84), mentions a deposit from which Mr. Allen sent fossils, and
says, “‘ The deposit is described as being about thirty miles east of
Warrnamboul, extending along the sea-coast for a distance of from
six to seven miles, and is from thirty to forty feet in thickness.” A
letter I wrote to Mr. Watts, on the possibility of its finding him, has
elicited no response; and I therefore presume that he must be
dead or have removed, and fear that the exact locality will not now
be discovered. ;
From the memoirs of the Geological surveys I conclude that it
will be found to be what the Australian geologists call Miocene, though
as yet this has not been shown to be of the age of the European
Miocene formation. Mr. Etheridge, Jun., writes that Allen pro-
spected in the ‘“‘ quartz cement which was considered by McCoy of
Pliocene age,” and says “ the country traversed by Allen and party
also consisted, especially near the coast, of beds which were referred
by McCoy to the Miocene period.” Mr. Etheridge, Jun., thinks pro-
bably the material marked Yarra-Yarra came from these beds, and
there is reason for supposing that the material was not quite
correctly labelled. The fossils which have been found in Muddy
Creek, Hamilton, Victoria, seem to support the Miocene age of the
beds; and similar Miocene clays, according to the Survey, occur in
several places, as near the mouth of the Aire river and also near
Geelong.
Besides the Bryozoa, I found a large series of Foraminifera very
well preserved; and I spent much time in picking out a large num-
ber, probably representing 50-100 species, which I forwarded to
Professor Karrer of Vienna, from whom I hear that he hopes to
complete the examination of the series this spring ; and I anticipate
that they will throw some light on the age of the formation, as
the Foraminifera, both fossil and recent, have had much more
attention than the Bryozoa. There were also a number of long slen-
der Jsis-joints, which I submitted to one of our authorities without
Q.J.G.8. No. 147. 4
SWO) A. W. WATERS ON FOSSIL CHILOSTOMATOUS
any result. The few molluscan shells are probably fry, and do not
give much assistance, but support the ‘“‘ Miocene” age of the beds.
There are also a few Entomostraca.
The fragments of Bryozoa are small; but their state of preserva-
tion is often very perfect ; and in this lies their chief value. Their
examination may well be used as an introduction to the study
of the Mount-Gambier series of Australia, in which, so far as I am
able to judge from the London Geological Society’s collection, kindly
lent to me, and trom a collection belonging to Mr. Etheridge,
jun., alsoim my hands, the state of preservation often does not
admit of the details being seen; so that the determination and de-
scription of these is sometimes very unsatisfactory if other material
is not at hand to be used as a key to the structure. As examples I
may mention Mrcroporella yarraensis, M. violacea, var., Porina cly-
peata, and Retepora rimata, which occur in the Mount-Gambier beds ;
but the details are wanting, and were it not for the “ Yarra-Yarra”
specimens I should have been unable to classify them.
The living British Bryozoa have recently been reclassified by
Mr. Hincks, who has introduced in some sections an almost new
classification. Since the appearance of his work no paleontogical
papers of any importance have appeared; and it therefore becomes
necessary to consider how far this classification is applicable in the
determination of fossils; and it is here that we shall perhaps find the
weak point in the modern classification: but, on the other hand,
fossils more than recent forms show the utter unnaturalness of the
older divisions. Although generic determination will often be diffi-
cult, that is by no means confined to the present system ; for we often
find fragments showing many important characters without being
able to distinguish if they have grown in the Hschara or Lepralia
form. Every change of classification should, of course, aim at
making the system more natural; but at the same time special
attention should be given to those characters which can be distin-
guished in fossils, seeing that the number of known fossil forms is
so many times more than all the known recent ones, and ultimately
the relationship of the living ones must be worked out largely by
means of the paleontological 1 record.
In the classification used by Busk in his ‘Crag Polyzoa,’ and, with
some modifications, by Reuss, the form of the ‘colonial erowth was
made the first consideration ; so that colonies of cells of ‘a certain
form incrusting stones or seaweed were called Lepralia, while quite
similar cells, growing back to back, forming an erect coral-like
stem, would be called Hschara or, if there was only one layer,
Hemeschara. With more careful examination and comparison of
recent and fossil forms this was found to be an absolutely untenable
position, as the same forms of cells so frequently occur that any one
well acquainted with recent and fossil Bryozoa could in a short time
draw up a list of at least 40 or 50 cases where absolutely identical
. cells are known in the Lepralia and Eschara forms. Smitt*, recog-
* Krit. Fort. ofver Skandinaviens washichhote se af F. A. Smitt. Ofv.
Vet. Ak. Forhandl. 1864-1868.
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. Olt
nizing this, based his classification mostly upon the form of the oral
aperture; and Mr. Hincks has followed Smitt’s example, introducing
some modifications. But sometimes there isa peristome obscuring the
oral aperture; so that it is difficult even in recent species to see the
shape of the real aperture, unless there is sufficient material at hand
to make the necessary preparations. As an example, in Tubucellaria
cercoides, Ell. & Sol., the operenlum which closes the primary aper-
ture is situated at some distance from the end of the peristome,
which is produced into a long tube. In fossils, however, it is
sometimes impossible to make out the exact form of the opercular
aperture, even when other details are extremely well preserved ; for
an example of which I only need refer to Porina clypeata (Pl. XVI.
fig. 67), in which the details are so well preserved that I think there
is no doubt it can be easily recognized when found elsewhere.
Probably no naturalist at all thoroughly acquainted with the
Bryozoa will again attempt to sustain such genera as the old Lepralia
and Eschara ; but it may be well to examine carefully the growth of
the Bryozoa before we entirely reject the form of the colony as of
elassificatory value ; for in many cases it may be shown in this way
from which part of a zocecium the following zocecium grows. The
mode of growth of Lepralia and Eschara indicated no structural
difference ; for the young zocecia in both grew out from the same part
of the parent cells, and Hschara was only formed of Lepralia-cells
back to back, often very slightly attached. For an example of the
new zocecia arising in a different manner we may cite Bicellaria
and Bugula, and fig. 33, provisionally placed with Cribrillina as C.
dentipora. The form of the aperture must be the first consideration ;
but especially among fossils we must carefully notice how they grow ;
and it is to be hoped that this latter question may soon receive a
thorough and conscientious investigation, as it is a point requiring
still further elucidation. At one time I hoped to be able to devote
some time to this question, which must be a laborious one; but I fear
the state of my health will not allow me to carry it out.
If the principles of the old classification had been adopted, it would
have been necessary to make several new genera; but workers on
recent Bryozoa have already overthrown the classification based upon
the zoarial form, and therefore paleontologists should follow Smitt,
Hincks, and others, and describe their species in such a manner,
and use such a nomenclature, that fossils can be compared with
living species.
The Australian Bryozoa, both recent and fossil, have been as yet
very imperfectly worked out. The most important works concerning
living forms are Macgillivray’s* papers, and, for the Catenicellide,
that of Prof. Wyville Thomsony. Prof Hutton has drawn up a list
* MacGillivray, P. H., ‘‘ Notes on the Cheilostomatous Polyzoa of Victoria,”
Trans. Roy. Soc. Vict. pt. ii. vol. iv. 1860; id. “ Descr. of some new Genera and
Species of Australian Polyzoa,” loc. cet. vol. ix. 1869; id. in ‘ Prodromus of
Zoology of Victoria,’ edited by F. M‘Coy, decades iii. & iv. 1879.
t+ Wyville Thomson, ‘‘On new Genera and Species of Polyzoa,” Zool. Bot.
Assoc. Dublin, vol. i. 1859.
y¥2
312 A. W. WATERS ON FOSSIL CHILOSTOMATUUS
of the New-Zealand fauna ; but, as he does not seem to have devoted
himself much to the Bryozoa, we cannot make comparison with the
New-Zealand species until some specialist has worked at them *.
There are several species described by Busk and Hincks in their
papers and works; and lately the study has been taken up by Haswell,
Goldstein, Maplestone, and J. B. Wilson, with interesting results.
The fossils have attracted comparatively very little attention. In
1859 the Council of this Society admitted a Note + by Mr. Busk on
Mount-Gambier fossils ; but this only consisted of a list of 37 species,
32 of which were new and were not described, but only christened ; —
so that it still remains perfectly useless for comparison. These names
have sometimes been quoted ; and workers have wasted their time in
libraries searching for the descriptions; and in the various biblio-
graphical and specific lists published by Mr. Etheridge, Jun., these
names are all referred to in full, and thus some pages are filled up
with empty names. As Stoliczka points out, such anticipatory pub-
lication brings confusion without equivalent advantage; and cer-
tainly in this case there has been much irritation and ink wasted,
which might have been avoided if the paper had been entirely ig-
nored. In Mr. J. E.T. Woods’s “Geol. Observations in Australia ”
entirely unsatisfactory figures without description appeared ; and
since then Mr. Woods has published a few short papers, to which I
refer in the descriptive text, of which I will only mention his paper
“On some Tertiary Australian Polyzoa” and “Australian Selenariade,”
in which fossils from Mount Gambier and Muddy Creek, Hamilton,
Victoria, are described, both being considered of the same age.
Therefore we may say that, with the exception of the papers by Mr.
Woods and one shortly to be mentioned by Mr. Wilson, no work has
been done on the Australian fossil Bryozoa; but in the description of
the Novara Expedition, vol.1. pt. 2, an important paper is published
by Stoliczka + on the Bryozoa from the marine beds of the Waitemata
Schichten of Orakei Bay, New Zealand; and as eight species are
common to both formations, the two deposits are of somewhat the
same age. ;
At the time I commenced the study of this material no fossil
Catenicellidz were known; but since mine were lithographed, Mr.
J. Bracebridge Wilson § has described and designated by numbers
twelve species, with none of which am I able to identify any of my
species. But the characters on which Catenicelle must be grouped
are as yet scarcely understood; and much change must be made in
the classification, as undoubtedly some of the names now in common
* BF. W. Hutton, Catal. of Marine Mollusca of New Zealand, Wellington,
1873; id. ‘‘Corrections and Additions to the List of Polyzoa in the Catal. of
Marine Mollusca of N. Zeal.,” Trans. New-Zealand Inst. voi. ix. 1876.
+ “Note on the Fossil Polyzoa collected by the Rev. J. EH. Woods near Mount
Gambier, South Australia,” by George Busk, F.R.S., F.G.S., &c., Quart. Journ.
Geol. Soc. vol. xvi. 1860, p. 260.
t Fossile Bryozoen aus dem tert. Griinsandstein der Orakei Bay bei Auck-
land, von Dr. Ferd. Stoliczka, 1864.
§ ‘* Fossil Catenicellze from the Miocene beds at Bird Rock, near Geelong,”
Journ. Micr. Soc. Victoria, vol. i. nos. 2, 3, p. 60.
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. ols
use are synonyms. As with other Bryozoa, so in Cuatenicella, the
form of the aperture will have to be considered of primary impor-
tance. This Mr. Wilson does not seem to have appreciated ; for
only in one case does he mention the shape of the aperture, and,
while in some the shape may not be distinguishable, we can hardly
suppose that all the twelve are so badly preserved as to have this
principal character destroyed. 1 have recently found two species
of Catenicella in the Geological Society’s collection from Mount
Gambier. Itis therefore notimpossible that when the figures which
' Mr. Wilson promises are published, one or two may be found to
occur near Geelong and in the present locality.
One most extremely interesting form—=indeed, the most interest-
ing specimen in the collection—is Catenicella internodia (fig. 78),
consisting of long internodes with a double row of cells, whereas all
the Catenicellidze now living have short beaded internodes, consisting
of one, two, or even three cells; and we may find that forms with
one or two cells in a node have developed from multicellular nodes,
and should then ask, have not all jointed forms adapted themselves
from unjointed ones? This and the Mount-Gambier collections
furnish unjointed Crisiw. In the living fauna of Australia the
number of jointed forms is very remarkable; but already in the
European Chalk the number was very considerable.
The Microporellidz are well represented, and also show that the
genus Microporelia must be extended; for we are able to trace rela-
tionship from WM. violacea, with a round pore, to the var. fissa, with an
elongate pore (fig. 73); then we have M. yarraensis, with two or three
denticulated pores in the depression ; and in this way pass on by .
coscmopora and var. armata, to M. symmetrica (fig. 83). This group,
with an area with several large pores, was well represented in the
Hocene and Miocene of Europe by M. coscinopora &c.; and perhaps
as the recent forms are further studied we shall find several living
allies; for Microporella (Kschara) distomu, Busk, from Madeira and,
in my collection, from Capri, from 150 metres, must evidently be
looked upon as related ; and I find in my specimens from Capri that
the pores are stelliform, which seems to be a frequent if not general
character in the group, and is of great interest, as showing a corre-
lation of characters, and supports the opinion of those who believe
that we are now on the track towards a more natural classification.
From the above remarks it will be judged that Porellina, Sm., which
is separated from the other Microporellide in consequence of having
the pore in a lunate form, is not considered a necessary genus.
If the comparison is extended a little further we may find that
such a form as M. symmetrica (fig. 83) is related to the Cribril-
linidee through such forms as C. terminata (fig. 68).
In studying both recent and fossil forms I have often been im-
pressed with the frequency with which open pores are replaced by
avicularia, and think that it is a matter worthy of most careful
examination ; and, considering that there is reason to believe that
avicularia may be only differentiated pores, I enter into the question
when speaking of Cribrillina suggerens.
314 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
The number of species of Chilostomata mentioned in this paper
is seventy-two; and, so far as my preliminary examination goes, it
seems that there are about thirty determinable species of Cyclosto-
mata; so that from this one small lump of clay there cannot be less
than two hundred determinable species when we add together
the Bryozoa, Foraminifera, Hntomostraca, and other remains. It
now becomes necessary to make comparison of these Chilostomata
with those found in other strata; and we find that a large propor-
tion are identical with those from the Orakei-Bay beds in New
Zealand. Stoliczka’s descriptions and figures do not in all cases
permit of comparison; but out of a total of twenty-nine comparable
species, there are from Yarra-Yarra seven Chilostomata and seven
Cyclostomata. With the Mount-Gambier beds the number is large ;
but this is the result of direct comparison, whereas I have had no
opportunity of seeing any fossils from Orakei Bay; and the number
of species from Mount Gambier, known to me, and of which I hope
shortly to publish a list, is greater than the Orakei-Bay list. The
number of identical species from the two places is now twenty-three
Chilostomata; but as I progress with the determination of the
Mount-Gambier collection the number will no doubt be increased.
We miss from this locality the Mount-Gambier species Cellaria
(Melicerita) angustiloba, Busk, and Spiropora verticellata (a species
common in the European Chalk). The C. angustiloba may be re-
presented by C. globulosa.
Twenty-two of the Chilostomata are known recent; and many
more are very nearly allied to living forms.
Three species are already known in the Miocene ? Muddy-Creek
(Victoria) beds, and four Chilostomata and, at any rate, three
Cyclostomata from the Hocene of Italy; but several others show
relationship to the Miocene and Kocene forms, and we are frequently
reminded of European Cretaceous ones, though in only one case
could we feel justified in identifying the species with any from the
Chalk.
It will, however, be well to defer further comparison until the
list of the known Mount-Gambier species, upon which I am now
engaged, is completed.
T have already * referred in various places to my reasons for ae
the term Bryozoa, which is now universally employed by German,
French, and Italian authors ; and Ido not therefore need to enter again
into the question. And although I am sorry that those few English
authors who have been before the public for a long time have not
been induced to change the name which they have used for several
years, yet I have indications which cause me to feel quite confident
that the next generation of English workers will use the class name
which has been employed in the rich literature of Germany and
France ; and I am glad to see that Mr. Tenison Woods 7 has begun
* “On the Terms Bryozoa and Polyzoa,” Ann. & Mag. Nat. Hist. Jan. and
Feb. 1880; ‘“ Reply on the Term Bryozoa,” ibid. Aug. 1880.
t “Corals and Bryozoa of the Neozoic period in New Zealand,” Palzontology
of New Zeal. pt. iv., Colon. Mus. & Geol. Surv. Depart. 1880.
| 8. Miicrepora patula ...........-...........- 326)...
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 315
to use this name, and to hear from Australia that it is there likely
to immediately replace the term Polyzoa. It is therefore with
much pleasure that I use the name in this contribution to the
paleontological literature of that continent.
Though considering that modifications of the definitions of some
genera is required through specimens now found, I leave that until
I have completed my examination of the Mount-Gambier collection
now in my hands.
The figures are all drawn with the camera lucida, and, as far as
possible, magnified twenty-five times; but this is in each case stated
by the side of the figure. I regret that Plates XV. and XVI. are so
unsatisfactory through want of success in transferring the drawing
to the stone; and, in fact, Plate XVII. came out so badly that I
was obliged to have it very considerably touched up upon the stone,
and much detail is thereby lost or altered. The Plates are also un-
satisfactorily arranged, in consequence of my receiving the material
at various times.
List of Specves.
=
a| 2
o © A Allies and Localities.
Sie 5 |
3 2 )S18
| Jae 1S
1. Catenicella cribriformis ............... 317
2. PERO oo aloe cidennsiinscocs i,
Pe MATSINALA... 2... cesses eeseeess a
4. FUDGE: penebets= Sele see eee eee »> |---| % |...| C. ventricosa, B., living.
5. PMR PAMEPHILONUSS on. os0cécccscness sss » |*|*|...| Australia.
6. elegans, var. Buskii, Th. ...... me selec eAcustralia:
ie SC_L13, Sosueucolee 318
8. BRERORILOO =< ja. 0 0022 ote cece aces -
Me@elaria tistulosa, L.................0000- 319) x | * |...) Miocene and Eocene of Europe.
10. MEAVEVONISIS. B.- 5c e.-ccoleec tos 321} «| *|...| Falkland Islands.
11. qricelloces Si ee ee »» |---| * |] C. tenuirostris, var. a, Busk.
12. 2.0 CLS) ceecgeeeee Pa oe eae ...| Eschara aspasia, d’Orb., Cretaceous.
9) ORT gS B22)|...|
mt. Caberea rudis?, Bush .................- » |*|...|...| Bass’s Straits.
} 15. Membranipora lineata, Z. .....,...... 323) x |...|...] Widely distributed.
| 16. catenularia, James. .........00008. », | ¥|---|:-.| Pliocene.
Lid iG 5, |---| ¥|...| WM. Flemingzi, living.
. —— macrostoma, RSs...............008 ,, |...|%*|* | Bartonian, Italy, and Miocene.
ILD. Ce B74 doe sal bee Cretaceous.
fe —— CONCAMECY ALA ..-.... 2.20202 -seneeces a
see LS 2 a ta Nellia simplex, B., living.
B —— maorica, Séol. ..........c.cec.cee0s 325| x |...| «| Upper Eocene, New Zealand.
SEL LTUC. 6 eee eee
316
A. W. WATERS ON FOSSIL CHILOSTOMATOUS
List of Species (continued).
S
Pale
a |=
|CR Allies and Localities.
. | alo
o |S] 35 |
a Le ios
AY Hie |O
25. Cribrillina terminata .................. 5 VA dllaaeload bec Lepralia scutulata, B., living.
26. denbiporayactcet seo ee i
27. Sugm@erens |: /.6 4. sscaseee eee 327 Cribrillina tubulifera, Hincks.
28. Mucronella mucronata, Sm. sae gnats 328] x | x |...) Florida, living.
29. duplicatal nots neeeee se ee ,, |*|*|...| Lyall’s Bay, New Zealand.
30. —— elegans, Macg. ...............000655 329|%?
ole Micropotella violacea, var. fissa ...... » |*|*|...| Indian Ocean.
32. ferbeal Beare eee ome eet ke 330)...| *
Do.) ——— Cleyata Hy GOGS ys eae een eee Pree tee
34. ———— Varraenmsiseensss essence eee dol}...| *
30. ———— COSCINO POA) eaeee-eseteeee encase a :
36. —— eNIGMAatICA ...........eceecceveeees ei
Ol. ———" SY MNMEGLICA) |. 252.56 son scsseoncccees 332
38. ClavabapSCOlsoun co eneeenen omen uid tenes *
oo. Porinds chy peata erect eee eee 1. | %
40. CORE JHU: soepcsbdacsosadesaes 333| «|x| *| Low. Hoc., New Zeal., Bart., Italy.
4], columnata RRM ited bane AL ce oh Sie esallccalicae Eschara heterostoma, Rss., Hoc., Italy.)
42. Lepralia corrugata) 222-22. -0--0-6--0--2 335 |
43. monilifera, var. armata ......... a0 bee ae ee Pliocene of Europe.
44. ——'spatullatan ce isseecmscnaee .ea eae »» |---| * |---| L. muléespinata, B., Madeira.
45, cleidostoma, Sm., var. rotunda |336|*?}...|...| L. elecdostoma, Sm., Florida.
46.- Porellajemend@atay.......-.ess0-scen enone P
47. denticulatas Stor. ss eee ss x |
AS. (Smibtiareentralagieey acre erst ood
49. -——— centralis, var. levigata ......... 5
50. Mater: EV OOS ik vce aes Sellen tise
1. aNCepS; ACh All sees caeceeeee near sre
52. Schizoporella vigilans .................. 538
538. phymatophora, Rss. ............ sp lescleeeiee .| Hocene of Italy.
54. ventricosa,, Flasw:\ i.e..ssscseeee Paleo |
55. === denestratays. 2700255..caescnnesee dence 309
56. SB) Dslaae Shosenadsognaeec saonnogsocbone: 5 |
57. SPi sessment meena cen en scen Leys lle ..| S. btaperta.
D8. —— submersa ............ccseeceseneeees 340 |
59. a= CONSOR Vata: (ci cccscocsconsockecenee RS *
60; ———Ispiroporinapeeseeee eee cee a;
61, ——‘excubans oe ae ee eee io41
62... amphora ane ee 3
63. AUS CALS aL OOO Seana eae nee ow glazelsee ...| Muddy Creek (Miocene ?).
64. Retepora marsupiata, Sm. ............ 342) x | « |x?| Miocene (America).
65. PUNUAGS Pa clsct tow aneenac soa ae 343]...| x
66. Cellepora yarraensis................---.- A
67. fossa, (ast a Ree eee iH x
68. fe UR abies so aauee tacts esi at Seen’ SY 0 a oe C. pumicosa (B., non Linn.).
69. Lunulites guineensis, Bush ............ ies
70. cancellata., Business cr ereenee eae
71. Selenaria marginata, T. Woods ...... ae
72 ailatia. Lio WOOdS\ie eins eee Sisal lege eos Muddy Creek (Miocene ?).
Lod
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 33)
1. CATENICELLA CRIBRIFORMIS, sp. nov. Plate XVI. fig. 39.
Zocecia wide, globose, with cribriform area below the aperture,
with five pores on each side; large lateral avicularia (wings broken) :
linear vittee nearly to the base; aperture rounded above (broken
below, probably straight) ; reverse smooth.
This is larger than C. hastata, and has more pores; and the lines
in the cribriform area are smaller.
2. CATENICELLA FLEXUOSA, sp.noy. Plate XVI. figs. 40, 41.
Cells elongate, irregularly oval, large depressions above and at
the side of the aperture; cribriform area small, with nine pores
(fenestre) ; aperture rounded on the distal edge, straight below. A
wavy thick tube on the front, which may be abnormal; reverse
smooth, raised over the upper and lower part of the first zocecium
and over the second zocecium.
This has some of the characteristics of C’. alata, Thoms.; and, with
only the one imperfect specimen, it is doubtful if it should be de-
scribed as new.
3. CATENICELLA MARGINATA, sp. nov. Plate XVI. figs. 44, 45.
Zoecia nearly cylindrical, a coffin-shaped margin round the
zocecium, and marginal bands enclosing depressions near the aper-
ture of the corneous joint ; aperture rounded above, doubtful below,
seven distinct pores surrounded bya line; back smooth.
4, CATRNICELLA AMPLA, sp. nov. Plate XVI. figs. 46, 50.
Cells large, subovoid, nine large pores (fenestre) on the border oi
a large area (scutum); small longitudinal ridge above the aperture,
with a depression on each side of it. Oral aperture rounded on the
distal edge, proximal edge somewhat arched. Dorsal surface with
a large grooved depression over the centre of each zocecium ; and by
the side are two long adjoining chambers, which are probably covered
by a membrane when living.
The lateral chambers are very characteristic, and somewhat re-
semble those in C. ventricosa, Busk; but in ventricosa they are
lateral but turned partly towards the front, while in the present
case the direction is dorsal. There is a faint median line, and
lines branching off to each fenestra, which are not shown in the
figure in consequence of the lithograph being badly put on the stone.
Loc. Mount Gambier (Lond. Geol. Soc. coll.).
5. CaTENICELLA aLata, W. Thoms. Plate XVI. figs. 47, 49, 53.
Catenicella alata, W. Thoms., “On new.Genera and Species of
Polyzoa from Coll. of Prof. Harvey,” p. 80, pl. vi. fig. 4 (Zool. Bot.
Assoc. Dublin, 1859, vol. i.).
Loc. Living. Fossil, Mount Gambier (Lond. Geol. Soc. coll.).
6. CATENICELLA ELEGANS, Busk, var. Busxir, W. Thoms. Pl. XVI.
figs. 42, 48.
Catenicella Busku, Wyville Thomson, “On new Genera and
318 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
Species of Polyzoa from the Coll. of Prof. Harvey,” Zool. Bot. Assoc.
Dublin, vol. i. 1859, p. 83, pl. vii. fig. 2.
Cells almost cylindrical, contracted towards the base. There have
been avicularia at both sides above the aperture. Aperture not
perfectly preserved, rounded on the distal edge, with a constriction
on each side near the base ; proximal border (smaller than figured)
slightly rounded. Vitte distinct, with double row of pores in a
depressed area.
The vittee of the Oreaee are not correctly figured and deseri-
bed in the British-Museum Catalogue; for, instead of being raised
areas with raised warts, they are sunken areas enclosed by raised
edges, and along these sunken areas there are one or two rows of
pores, according to the species. The vitte, however, when covered
with a membrane, may appear like raised areas ; but anexamination of
the British-Museum specimens shows that the structure was not quite
correctly appreciated, and it would be a great advantage if any one
who undertakes the revision of the Catenicellide would give figures
with all the membranes removed. The size of the recent and fossil
species is identical.
In order to compare Catenrcella, Scrupocellaria, and other more
or less corneous forms, I made a series of calcined preparations of
most of the recent specimens in my possession.
This is allied to C. perforata, B
Loc. Living; Bass’s Straits (7.), Australia (my coll.).
7. CATENICELLA SOLIDA, sp. nov. Plate XVI. figs. 37, 38.
Single cell oblong to cuneate, double cells ovate to globular; a
straight band or ridge down the front of each cell, and a similar
raised band separating the two zocecia ; a small curved ridge forming
a circle on each side of the aperture, and below the aperture a linear
band on each side. On each side of the central bands large pores
(sometimes double pores). Oral aperture round above, with a small
sinus on the proximal edge; a denticle on each side of the top of the
sinus. Dorsal surface with several large depressions, bounded by
bands similar to those on the front ; the bands, both front and dorsal,
are grooved. Avicularia very minute, angular or rounded (about
half the length of the oral aperture), on the side of the cell near the
distal end.
This is common in the Yarra-Yarra formation, where, however,
the cells are usually found double, and the number of single cells
seen is very limited. The bands vary somewhat in shape; but fig. 38
_ shows the typical form. This has many points of relationship with
C. ponderosa, Wilson (Micr. Soc. Vict. vol. 1. p. 63, pl. v. figs. 1-
3), a living species; also with C. carinata, Busk; and C. species xii.
of Wilson (loc. cit. p. 63), a fossil from Spring Creek, but I am
unable to identify it with any described species.
8. CATENICELLA INTERNODIA, sp. nov. Plate XVI. figs. 78, 79.
Zoarium in distinct internodes of several zocecia arranged in a
bicellate series. Zocecia suboblong, with a wide ridge down the
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 319
middle of the zocecium ; the band spreads out at the top immedi-
ately below the aperture in an oval form, causing an oval depres-
sion surrounded by the band. ‘The upper part of the zocecium,
comprising the aperture and this oval, is slightly raised; in the
longitudinal depression four or five pores. On the inner side of the
zocecium, above the aperture; a small flattened boss; on the outer side
a small triangular avicularium ; a large depression or pore in the
middle of the central band. Oral aperture semicircular, with the
proximal edge straight; on the back an irregular oval depression
behind each zocecium, with from three to five pores in each of these
depressions.
This is allied to C. solida, Waters (figs. 37, 38); but the shape of
the aperture is different, besides considerable difference in the
structure of the back. At first I thought the large holes in the
middle of the centre band were accidental; but this is really not
the case, as in the cells, when there is no hole there, it is replaced
by a dark round spot, probably of thinner shell.
9. CeLtaria FistuLtosa, L. Plate XIV. figs. 1, 2, 10, 11.
Cellaria fistulosa has occasioned systematists the greatest difficulty ;
and it now possesses a mass of synonyms (for which see Hincks
and Reuss), of which many can never be compared. When
J examined these and the allied species from this Victorian mate-
rial, I at first felt that it would be impossible to separate them,
and thought with Reuss that the range of variation was so great
that such forms as C. fistulosa, sinuosa, crassa, marginata, &c. must
be included under one specific name. Since my preliminary exami-
nation My. Hincks’s most valuable work on the British marine
Polyzoa has appeared, in which he distinguishes three species,
fistulosa, sinuosa, Johnson. I have therefore, with this book before
me, again very carefully examined my recent specimens, first cal-
cining considerable portions; and the conclusions I have come to
are :—that the shape of the cell is so variable that it is perfectly
useless as a character (this has already been mostly recognized by
recent writers, but was the character on which the species were
some time ago principally founded); then I next found that the
bordering rim, which is a character of C. Johnsoni, Busk, is some-
times found on one part of a colony of C. fistulosa, and absent in
other parts; next I found the shape of the ovicellular opening
equally unsatisfactory (for in most undoubted specimens of jistulosa
from Naples it occurs in some cells as a minute orbicular opening,
then it is elongate oval, and in other apparently older ovicells a broad
semicircular line is formed, which changes to a transversely oval
opening, resembling that figured by Mr. Hincks as a character of
C’. sinuosa). In the same specimen, before any ovicells are formed,
the aperture is very near the top of the zowcium; but afterwards
its position is near the centre. Having found the position of the
aperture, the shape of the ovarian opening, the shape of the
zocecium and of the bordering rim unsatisfactory characters, there
only remained the avicularia; and in all the specimens I have ex-
320 A. W. WATERS ON FOSSIL CHILOSTOMA TOUS
amined I have found one form constant: the jistulosa from the
Mediterranean has its rounded avicularium above the zocecium ; the
stnuosa has a diagonal avicularium pointed downwards, with the
lower part raised; the Johnsoni, from Rapallo (Italy) and New
Guinea, has a zocecial avicularium with a projecting hood above,
as figured by Hincks. I find my observations on the recent species
entirely confirmed by the examination of a large number of fossil
forms.
Some thick specimens, such as fig. 1, have the characteristic avicu-
laria of the European jistulosa ; these are somewhat rare ; but slender
specimens, such as fig. 1Z, are common, and probably these are the
same species; but as I have been unable to find any avicularia in
these, both from Yarra-Yarra and Mount Gambier, the point can-
not be decided with certainty. In the specimens figs. 10, 11, how-
ever, I find a small wide avicularium, as in larger fistulosa, with
which these must therefore be united. The shape of these last
resembles that of C. Johnsont, which is the C. marginata, Reuss
(Lert. Wien, p. 59, pl. vu. fig. 29, not 28); and I have slender
C. Johnsoni from off Raton (New Guinea) resembling figs. 10, 11
in all except the avicularium, which is the large rounded one with
which we are already acquainted in C. Johnsonz.
In fig. 11 we have an interesting specimen, as showing how very
slender they may sometimes be; this has only one longitudinal
row of cells on each of the four faces. In specimens from Mount
Gambier, like my fig. 12, I have occasionally found in the oral
aperture two teeth above and two teeth below, and in the ovarian
openings sometimes one set of teeth, sometimes two; but these
cannot be looked upon as constant characters, and lead us to think
that C. crassa must be considered a doubtful species; or perhaps
two species are represented, seeing that avicularia of two kinds
are figured. I also sometimes find in the recent C. Johnsoni, from
Rapallo, two such teeth in the upper part of the aperture, as well as
the two below.
Fig. 1 shows that the joints of this specimen were attached by nu-
merous horny tubes. In recent C. tenurrostris and C. malvinensis the
joints are usually thus attached ; but this is not the case inC. fistulosa;
but in specimens of C. Johnson, from Rapallo, there are sometimes,
though not usually, several such connecting tubes. This leads us
to the consideration of these joints; for when a stem divides and
two new branches are formed, the calcareous wall is continuous,
and in some the branches are already large (perhaps throwing out
fresh branches) before this calcareous wall is broken through. Of
specimens J examined, I found this calcareous structure remained
continuous longest in C. Johknsonz, but scarcely at all in C. gracilis,
while C. fistulosa occupied a mean position; hut much might de-
pend upon the sea in which each specimen grew, as jointed structure
in this and other genera must be looked upon as an adaptation to
moving water. In fossil specimens from the Pliocene &c. perma-
nent ankylosis, as already pointed out by Busk and Hincks, is
frequent. I‘am not inclined to think that, as a rule, articulation
tl er
;
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 321
can be made a basis of generic classification; and perhaps at some time
the geologival record may show us that jointed forms are all derived
from unjointed ones.
Loe. Living, widely distributed. Fossil: Mount Gambier, com-
mon ; and also from the Miocene and Pliocene of Europe; but as we
cannot be quite sure from the descriptions of Reuss and others that
Salicornaria farciminoides does not include other species, it is best
to refrain from giving localities.
10. Crttaria Matvinensis, Busk. Plate XIV. fig. 3.
Salicornaria malvinensis, Busk, Mar. Poly. p. 18, pl. lxiui. figs. 1, 2.
The zoarium is about the same size as Cellaria fistulosa, fig. 1;
sometimes the cells are hexagonal, at others more acute above and
below ; an acute avicularium replaces a zocecium. ‘The front of the
zoceclum is very much depressed, being surrounded by a raised bor-
der; distal edge of the oral aperture rounded, contracted above, so
as to suggest a subtriangular shape; proximal edge curved inwards,
with a small tooth at each side.
Loc. Living: Falkland Island, South Patagonia (Darwin). Fossil :
Mount Gambier, common (Lond. Gol. Soc. coll. & Eth. coll.).
11. Crtraria ovicettosa, Stol. Plate XIV. figs. 4, 5, 6; Plate
XVII. fig. 62.
Salicornaria ovicellosa, Stol. Foss. Bry. Orak. p. 151, pl. xx.
nes. 9, 10.
From Yarra-Yarra I have several small fragments; and in some
there is a rim round the cell, as figured by Stoliczka, and in others
it is plain, as in fig.4. The most interesting specimen is one in the
possession of Miss Jelly (fig. 62), which shows the great range of
variation and the great difficulty in determining species on the
characters generally used—as, for instance, the mouth varies in posi-
tion in the fertile and unfertile cells, and the zoarium, in this case,
is quite thin (as in fig. 4) in the upper and lower parts; but in the
middle the diameter is more than twice as great, and in this
thicker part, where the cells are fertile, there are very large acute
raised avicularia above the zoccium, occupying nearly as much
space as the zoecium. Fig. 5 shows the position of the distal
rosette plates, which are not quite in the centre of the zoarium.
Fig. 6 shows the two lateral plates on each wall.
This is evidently very closely related to Cellaria tenuwirostris
(especially var. a) of Busk, from Bass’s Strait, Tasmania, Florida,
&c.; butit differs in having the upper part of the avicularium much
projecting, and the rim is regular instead of being raised at the two
sides.
Loc. Orakei Bay, New Zealand (St.); Mount Gambier (Lond.
Geol. Soc. coll.).
12, CELLARIA GLoBULOSA, sp. noy. Plate XIV. figs. 16, 17.
Zoarium consisting of joints, from the top of which arise two
sunilar joints connected with the first by corneous tubes; internodes
OLE A. W. WATERS ON FOSSIL CHILOSTOMATOUS
short, laterally subcircular, compressed. Zocecia quincuncially ar-
ranged, hexagonal ; oral aperture arched above, lower lip straight,
with two distinct denticles, aperture placed one third the length of
the area from the top; zocecial area slightly depressed.
This differs trom Cellaria (Kschara) aspasia, d’Orb. (Pal. Fr.
p. 132, pl. delxvu. figs. 14, 16), in having the cells distinctly hexa-
gonal instead of spatuliform, and from Melicerita angustiloba, Busk,
in having the cells arranged quincuncially instead of in transverse
rows; consequently the distal borders are straight and in con-
tact in C. globulosa, while the lateral borders are straight in
M. angustiloba, B.
From specimens I have seen from Mount Gambier, Melicerita
angustiloba certainly seems to be a jointed species, and should be
united to Cellaria, The genera Melicerita and Hscharinella are
separated by d’Orbigny in consequence of the first having the cells
transverse, while they are quincuncial in the second. Latereschara
was also divided from Hschara on the same grounds.
Mr. Vine has in his possession a node from this locality, which is
very irregular and elongate.
13. Canpa FossILis, sp. nov. Plate XVI. figs. 51, 52.
Cells biserial ; aperture elongate, rounded above, contracted below;
upper margin recedent, with a spine on each side. Surface granu-
lated. An avicularium (or spine) on the inner side of each zocecium,
placed about one third of the length of the zocecium from the top.
On the side a large pore for tubular fibre, above which is a vibra-
culum ; on the dorsal surface cells arranged diagonally.
This much resembles Canda arachnoides, Lamx., but differs in
having a smaller aperture, and in the pieces found there is no
median avicularium ; but possibly this may exist, as the diagnosis is
based on a few small fragments. In C. arachnoides the cells on the
dorsal surface are parallel with the median line.’
Loc. Mount Gambier (Lond. Geol. Soc. coll.).
14. Caprrea rupIs, Busk?. Plate XVIII. fig. 86.
Caberea rudis, Busk, Cat. Mar. Polyz. p. 38, pl. xlvi.
Zocecia elongate, oblong; aperture elliptical, occupying about one
half of the front of the zocecium; area sloping inwards, very minutely
granular ; a spine on each side at the top of the aperture, and a small
opening (spinous or radicular) beyond the rim of the area; a small
avicularium on one side below the area. So-called operculum large,
entire, elliptical. Ovicell much raised, opening arched, rather flat-
tened in front, with a line round the flat region. A small avicu-
larium on one side near the top of the ovicell. ;
The fragment only consists of one row of cells; and therefore it is
impossible to be quite sure of the determination ; but if not rudis, it
approaches very closely to it, and the vibracula apparently cor-
respond.
The preservation of the operculum in so fragile a specimen was
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. O20
surprising ; but I have also a specimen of Caberea from Mount
Gambier with all the operculum remaining.
Loc. C. rudis is found in Bass’s Strait (B.).
15. Mempranrpora LInEATA, L.
I have a small fragment of Membranipora consisting of two elon-
gated cells with large area, with an acute avicularium above the
cell, with beak pointing downwards, about sixteen large spines
round the cell, and two smaller ones just above the border on the
distal extremity. This seems to vary from the living lineata only
in having more spines; but from so small a fragment it is impos-
sible to speak with certainty.
16. MEMBRANIPORA CATENULARIA, Jameson,
For syn. see Hincks’s Brit. Polyz. p. 134.
The specimens are small, consisting of only a few cells, but cor-
respond exactly with recent specimens | have from the Semaphore,
Adelaide, Australia.
Living: Northern seas, Brit., Medit., Canada, Australia, Fossil:
Pliocene of England and Italy. .
17. MemMBRANIPORA CYLINDRIFORMIS, sp. nov. Plate XVII. fig. 74.
Zoarium cylindrical. Zocecia not distinctly separated; area con-
tracted above, expanded below, filled in for about a third of its
length with a calcareous granular lamina. Aperture subcircular,
flattened below, margin much raised ; oral spines, two large and two
small ones; small acute triangular avicularium above the area, and
larger more elevated ones below placed transversely.
From the material marked “‘ Yarra Yarra” I have only found a
small piece ; but from Mount Gambier I have larger cylindrical pieces.
The form of the zocecia is very similar to that of M. Flemingi.
Loc. Mount Gambier (Lond. Geol. Soc. coll. and Eth., jun., coll.).
18. Mempranipora macrostoma, Rss. (in Vincularve forma). Plate
MVS figs. 13, 19.
Cellaria macrostoma, Rss. Foss. Polyp. d. Wiener Tert. p. 64,
pl. vill. figs. 5, 6.
" Biflusira macrostoma, Rss. Die foss. Anth. u. Bry. der Sch. von
Crosaro, p. 274 (62), pl. xxxiil. figs. 12, 13; Ak. Wien, vol. xxix.
? Biflustra papillata, Stol. Foss. Bry. Orak. p. 154, pl. xx.
figs. 14, 14a.
Flustrellaria macrostoma, Manzoni, I Brioz. foss. del Mioc. d’Aus-
tria ed Ungh. p. 67 (19), pl. xiii. fig. 46 ; Ak. Wien. vol. xxxvii.
Zoarium subcylindrical, or much compressed, a number of vari-
cells. Zocecium distinct, with a well-marked border. Aperture
elongate oval, occupying nearly the whole of the front of the cell;
sides of the area folded inwards, so that the aperture is in a deep
depression. Small raised avicularia above the zocecium in a hori-
zontal or diagonal position. Distal rosette plates two, near the front
of the distal wall.
324 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
Aperture 0:46 millim. long.
Loc. Oligocene (Bartonian), Val di Lonte (Ztss.), Brendola, Colle
Berici, Ferrara di Monte Baldo (A.-W.-W. coll.) ; Miocene, Nussdorf
(Manzon2), Orakei Bay (Stol.), Mount Gambier (Lond. Geol. Soc. coll.).
19. Mrempranipora AReus, d’Orb. (in Vinculariew forma). Plate XIV.
figs. 20, 21.
Vincularia argus, @Orb. Pal. Franc. p. 253, pl. delxxxix.
figs. 1-4.
Zoarium erect, slightly compressed. Zocecia quincuncially ar-
ranged in longitudinal lines, distinct, irregularly hexagonal, con-
tracted below, not raised above the general surface. Aperture oval,
occupying about one third of the zoecium. Two distal rosette
plates near the centre of the distal wall; lateral rosette plates
several close together (fig. 20, a).
This differs from M. macrostoma in having a very much smaller
aperture, which is not in so deep a depression. The aperture is
0-31 millim. long.
Loc. Cretaceous, Meudon (d’Orb.).
20. MEMBRANIPORA CONCAMERATA, Sp. nov. (in Vencularie forma).
Plate XIV. figs. 22, 23.
Zoarium slender, erect, hexagonal in section, dividing dichoto-
mously, about 0°5 millim. in diameter. Zocecia in longitudinal
lines quincuncially arranged, distinct, with raised border, concave,
elongate, contracted slightly below; border much raised above the
aperture, forming a raised arch. Aperture oval, occupying from one
third to one quarter of the length of the zocecium. Zocecial avicu-
larium at the junction of each branch. One distal rosette plate
near the centre of the zoarium (fig. 23); two lateral rosette plates
(fig. 22, a).
This is the most common fossil in the material, and much resem-
bles Vincularia gracilis, d’Orb., from the White Chalk of France,
but differs in being smaller and having a smaller aperture, and
having six cells in a series instead of eight ; but we now know that
this last is not an important difference ; perhaps the two should be
considered varieties of one species.
Aperture 0°14 millim. long.
21. MEMBRANIPORA LUSORIA, Sp. NOv. (in Vincularie forma). Plate
XIV. fig. 14; Plate XVIII. fig. 82.
Zoarium ep lind eal) jointed, dichotomously dividing. Zocecia
suboval, rounded above, contracted below, distinct, surrounded with
an elevated margin raised above the aperture. Aperture large, about
one third the length of the zocecium, oblong, rounded at the corners,
contracted towards the middle. Very large elevated zocecial avicu-
laria directed downwards, with acute mandible.
Aperture 0-2 millim. long, 0-11 wide.
The form of the cell suggests a battledore, or, better, snow-shoes ;
and therefore, finding some difficulty in giving a distinctive name not
Quart. Journ. Geol. Soe. Vol. MX PE
Mintern Bros , imp,
VICTORIAN FOS Sil BRVvOZzea.
A.W. Waters lith.
Quart. Journ. Geol. Soc. Vol. XXXVILPL XV.
“s
© a
Paap
eee wenss
2088S ny,
L2
,
& j
. » ae eee
Mintern Bros ,1mp-
A.W. Waters lith.
VICTORIAN FOSSIL BRYOZ (OVA
“a : a
Po by
~ *
+
oe
s
* f
- ri
{
é 1
oa ‘ s,
Quart. Journ .Geol. Soc. Vel. XXXVIL. Pl Vig t
Mintern Bros ,imp-
A. Waters lith.
FOSSIL BRYOZOA.
WACOM OITA
25
L
Mag.
Quart Journ. Geol. Soc. Vol. XXVIT. PL. XVIL.
Br tay
nce
4
reap
Mache & Macdonald imp.
AW. Waters, ith
VICTORIAN POSSI) BinwozZ Ose
—yr--
AW. Waters. lith.
Quart. Journ. Geol. Soc Val. XAVIT Pl VE
&
pee pen
Maclure & Macdonald amp.
VICTORIAN FO Soil, BRYOZOA:
BRYOZOA FROM §.W. VICTORIA, AUSTRALIA. 325
employed in this or neighbouring genera, I have allowed myself to
stretch a point in choosing a name. ‘This would belong to Wellia of
Busk; but that is a genus which, as defined, cannot possibly be
maintained, and the present species with zocecial avicularia shows
how unsatisfactory a character the absence or presence of avicularia
is. Nellia, Busk, is almost synonymous with Quadricellaria, d’Orb.
This is very closely allied to Nella simplex, Busk, from Prince of
Wales’s Channel, Torres Strait ; the aperture in that case, however, 1s
0-5 millim. long and a reguiar ellipse, while in M. lusoria it is only
0-25 millim. long. Fig. 14 was drawn from a worn specimen with-
out avicularia, before I had seen the one figured as 82; and then
I could not make out all the structure.
22. MemBranipora MAoRIca, Stol. (in Vincularie forma). Plate XIV.
fig. 9.
Vincularia maorica, Stol. Foss. Bry. Orak. p. 153, pl. xx. fig. 8.
Vineularia? maorica, Hutton, on some Austral. Polyz. p. 23,
Rep. R. Soc. Tasmania, 1877.
Vincularia maorica, T. Woods, “ Corals & Bryozoa of the Neozoic
period in New Zealand,” Paleont. of New Zeal., Col. Mus. & G.S.
Dept. 1880, p. 27.
Zoarium erect, with six cells in a series, or, thickening out, in
places there are eight. ocecia with a raised border, rounded, with
a tendency to be hexagonal, calcareous, front of the zocecia de-
pressed, two tubercles above each zocecium. Aperture (usually
rather larger than figured) slightly trifoliate, distal edge rounded,
and proximal edge straight. Avicularia large, occupying the place
of a zocecium. ‘Two round rosette plates near the middle of the
distal wall. (In the same position as shown in fig. 21.)
It is evident, from the description and the figure of the section,
that Stoliczka’s specimen was somewhat worn; and in such a case
the cells would assume an entirely hexagonal form. The presence
of the tubercles is indicated in his figure of the section. The avicu-
laria are the same as those so common in many of the fossil Mem-
branipore-—for example, M. angulosa, Rss. (see my figure in Bry. of
Bay of Naples, pl. xii. fig. 3, Ann. & Mag. Nat. Hist. s. 5, vol. ii1.);
and it is interesting to find this with a distinctly Vincularian mode
of growth. Smitt, when he broke up the old genera Lepralia and
Eischara, indicated the colonial form by adding “ Lepralia-, Hschara-,
or Hemeschara-forma”; and we may further extend the principle
by speaking of Vincularca-forma: thus the form of cell and the
generic relationship will be shown, together with the mode of
growth.
Loc. Living, Tasmania (Hutton). Fossil: Orakei Bay ; Hutchin-
son’s Quarry, Oamaru (New Zeal:); Upper Eocene of New-Zealand
geologists.
23. MEMBRANIPORA GEMINATA, sp. nov. Plate XVI. fig. 55.
I have only found a small fragment of this; but it seems to be
a branching form, with two cells diagonally to one side, followed by
Q.J.G.8. No. 147. Z
526 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
two cells turned towards the other side. Area an irregular oval, with
margin thickened, much raised, surrounded by numerous spines.
24, MicRopora PATULA, sp. Nov.
Zocecia distinct, divided by a scarcely raised thin border, sub-
quadrangular, finely granulated with small pores, more numerous
round the edges; distal portion of the zocecium much depressed,
raised above the distal edge of the aperture and forming a hood over
it. Oral aperture rounded above, straight below, with a much raised
lip or rim.
Aperture 0°25 millim. wide, 0°14 long.
This has some resemblance to Vencularia binotata and cucullata of
Reuss and Manzoni; but the fragment is so small that we do not
know if it grewin the Vincularia-form. The mouth is much larger ;
and also the zocecial border is less distinct.
Loc. Fossil: Mount Gambier (Lond. Geol. Soc. coll.).
25, CRIBRILLINA TERMINATA, sp. nov. Plate XVII. fig. 68.
Zoarium in the Hemeschara-form. Zocecia but very slightly raised,
the plain borders of neighbouring zocecia nearly confluent, so that
the divisions of the zoccia are scarcely visible; cribriform area
somewhat depressed, the large pores concentrically arranged. Oral
aperture rounded on the distal edge, straight on the proximal, con-
tracted below. Small rounded avicularium above the aperture,
a small one immediately below, a little to one side, and a small one
on each side, just below the line of the aperture.
Oral aperture 0-13 millim. wide at base, 0°17 at widest part,
0-18 long. ;
This seems to have much in common with Lepraha scutulata,
Busk (Q. J. M.S. vol. iii. 1855, pl. ii. figs. 1, 2); and it is difficult
to know where it should be placed, as the pores do not seem to show
any radial structure, and the aperture is contracted below, having
the same shape as the oral aperture of Diporula verrucosa. It also
has many points in common with C. punctata, and is one of those
types which appear to be connecting links between widely separated
forms.
26. CRIBRILLINA DENTIPOR, sp. nov. (in Bactridii forma). Plate XY.
fig. 33.
Zoarium erect, with zocecia only on the front; zocecia growing
from the side near the distal end of the zocecium below, the axis of
each zocecium being thus diagonal to each of its neighbours. Zocecia
with a large raised cribriform area, the pores being placed concen-
trically, each pore with a denticle pointing away from the centre of
the area. Oral aperture semicircular, with a straight proximal
edge, 0°14 millim. wide. A small avicularium directed outwards
on each side of the aperture. Dorsal surface with a central groove,
and smaller depressions on each side.
The fragments are small, and not sufficient to found a new genus
upon, which may possibly be necessary when large pieces are found ;
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. By247(
for the zocecia originating at the side is an important characteristic.
The form of the cell, however, very closely resembles that of Cri-
brillina terminata (fig. 68); and by the present designation we, at
any rate provisionally, show the zocecial relationship and the mode
of the zoarial growth. After finding that Schzzoporella phymatopora
(fig. 32) showed, when broken, a structure like Bactridium, I re-
examined the present fragments, which, however, seem to belong to
a form with cells on one side only, growing erect with only one
series of cells. The British-Museum specimen of Lepralia monoceros,
Busk, shows that the pores in that species also are provided with a
denticle ; but in that case the denticles are irregular.
27. CRIBRILLINA SUGGERENS, sp. nov. Plate XVII. fig. 75.
Zoarium in Aschara-form, consisting of two layers of cells grow-
ing back to back. Zocecia oval, distinct, quincuncially arranged, with
a double row of from twelve to fourteen erect tubular projections
on the front, and a smaller row on the side, and some smaller ones
in the central area ; large pores between the tubes. Oral aperture
small, semicircular, with straight proximal edge; in one case two
curved irregular spines form a sort of arch over the aperture. A
short triangular avicularium above the aperture on one side. Two
oblong lateral rosette plates, one oblong distal plate.
Proximal edge of aperture 0°06 millim. wide.
This is a most curious and instructive form, in which we are at
the outset met by a difficulty as to its generic position; for, looking
at the aperture, we find it might belong to Cribrillina or Mucronella.
With the latter, however, in other respects there is little in common ;
but with Crébrillina we find the radiating character of the pores,
and, although no known species has such a bristling surface, yet in
C. Gattye, C. cribrosa, Hell.*, C. figularis, &c. there is a row of
slightly raised pores round the edge of the cribriform area.
These very curious prominent tubes (about 0°07 millim. high)
naturally lead to the consideration of the signification of the pores
and of avicularia; for may not avicularia have originated in such
tubes having covers? and we may again ask, is the function of
these tubes different from that of the pores which we almost univer-
sally find on the surface of the Bryozoa? The physiological signi-
fication of these pores is, perhaps, not sufficiently appreciated ; and
therefore a moment’s digression is necessary, as we may thus have
the record even in fossils of physiological structure. When a recent
cell is decalcified, the membrane remaining shows small disks where
the calcareous pore has been, and a spot in the centre of this disk
further shows that to each one a thread of the endosarc has extended ;
so now we see that oxygenation, or a similar vitalizmg change, takes
place by means of the communication with the exterior through these
pores. The front of a cell, however, frequently becomes covered
with mud or organic growth; and in such cases raised tubes might
be of great advantage in the economy of the colony: and if these
* See my fig. 4. pl. ix. in Bry. of Naples (Ann. & Mag. Nat. Hist. ser. 5,
vol, iii. 1879), to which I have now to make addition. 6
Z
328 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
are provided with a lid or ‘“‘beak,” they may still longer render
assistance to the colony ; for the polypide of a cell may be dead,
and the cell itself covered with mud, but yet the zoarium may be
living, and under favourable circumstances a new polypide may
grow in this very zocecium.
Modifications may take place, and the avicularia become highly
differentiated, until we find them occupying the place of a zocecium
and of equal individual value with the zocwcia. Tracing it thus
from below instead of from above, as is usually attempted, we get
a much more reasonable explanation of the origin and function of
the avicularia; for certainly when we find very minute avicularia
on the root, andon the back of the zoarium, besides large numbers on
the front of the cell, the prehensile theory seems utterly to fail; and
although the present idea requires further development, yet the
examination of living forms seems to furnish much to support it.
Smitt points out that in Nellia oculata, B., the papilliform pro-
cesses are avicularia, sometimes with and sometimes without covers
(mandibles) ; and we are constantly meeting with similar instances.
Mr. Hincks has kindly furnished me with an advance plate and
description of Cribrillina tubulifera, Hincks (see Ann. Nat. Hist., .
July 1881, p. 8, pl. i. fig. 7), to which the present is closely related.
The only important difference seems to be the relative size of the
oral aperture, which is very small in the fossil. The specimen now
described is very small; and it is to be hoped that a larger specimen
may be found, upon which the affinities can be more exactly studied.
28. MucronELLA MucRonaTA, Sm. Plate XVII. fig. 66.
Kscharipora mucronata, Smitt, Floridan Bryozoa, p. 24, pl. v.
figs. 113-115.
? Eschara Lnversidge, T. Woods, ‘‘On some Tertiary Australian
Polyzoa,” Tr. Roy. Soc. New 8. Wales, 1876, p. 3, figs. 11, 12, 13.
Zocecia obscure, slightly elevated; aperture rounded above, straight
below, with a mucro or broad, flat, plate-like expansion in front of
the proximal edge; on the front of the zocecia usually five large
pores partially closed by a large, simple or bifurcate denticle, some-
times only three or four large pores, when there is usually a small
rudimentary pore. Angular avicularia at the sides of the zocecia ;
the two are usually unequal in size; a minute avicularium in the
aperture. Probably incrusting or Hemeschara-form, from Yarra-
Yarra. Aperture 0°23 mm. wide.
In the Mount-Gambier specimens in the Lond. Geol. Soe. collec-
tion there are usually only three pores, but sometimes four or five ;
and although the avicularia are not so distinct, and were not figured
or described by Mr. Woods, yet they are to be seen at the sides of
the zocecia.
Loc. Living: W. off Tortugas, Florida. Fossil: Mount Gambier
(Woods and Lond. Geol. Soc. coll.).
(29. MucRoneLna DUPLICATA, sp. nov. Plate XVI. fig. 54.
The fragment is small; but some characters are shown which are
BRYOZOA FROM 8.W. VICTORIA, AUSTRALIA. 329
important, and by which it may be recognized again should it be
found elsewhere.
The aperture is orbicular, with a mucro turning inwards over the
aperture. On each side, below the aperture, there is a large avicu-
larium, also one on each side two thirds of the distance from the
next aperture. Above the aperture there is a raised area with a flat
surface, apparently an ovicell. Above the ovicell and down the sides
of the zocecium there is a row of large pores.
The peculiar flatness of the ovicell is not shown in the drawing.
A specimen sent over to the British Museum by Mr. Hutton from
New Zealand, marked and mentioned in his catalogue as Lepralia
variolosa, seems to be this species. In the recent species the ovicells
have a small umbo, and there is not a second pair of avicularia
guarding the ovicells ; but the position of the upper avicularia is
the same, and the shape is similar. JV. duplicata also occurs from
Mount Gambier (Lond. Geol. Soc. coll.) with the zoarium erect, cy-
lindrical, with one cell turned in each direction.
30. MucroneLia ELEGANS, Macg., var.? Plate XVIII. fig. 91.
? Eschara elegans, Macgillivray, “ Austr. Poly.” Trans. Roy. Soc.
Vict. pt. ii. vol. ix. 1869, p. 138.
Zocecia quadrate, surface finely granular with pores, except just
below the aperture, a round avicularian pore immediately below the
aperture. Oral aperture rounded on the distal edge, the proximal
edge arched, forming a lip, a minute denticle on each side of the
mouth immediately above the angles. Aperture 0°17 mm. wide ;
0-1 long from the top of the lip to the distal end of the aperture.
Only two cells are preserved ; and therefore it is impossible to be
sure of even the generic position of the specimen ; but it is evidently
related to the species from Queenscliff and Portland Bay, described
by MacGillivray as Eschara elegans, a name that should not have been
given, as there is already H. elegans of Milne-Edwards. In #. elegans,
MacG., no suboral avicularia are mentioned; but according to Mac
Gillivray avicularia are sometimes situated at the side of the mouth.
31. MrcroporELLa vioLAceA, Johnst., var. rissa. Plate XV. fig. 26;
Plate XVII. fig. 73.
Microporella fissa, Hincks, ‘Contr. Gen. Hist. of Mar. Poly.,’
Ann. & Mag. Nat. Hist. ser. 5, vol. vi. no. xxxv., Nov. 1880, p. 381,
pl. xvi. fig. 4.
Zoarium in Eschara-form, flat, compressed. Zocecia pyriform
or oval, much raised, surrounded by a row of pores, or in old and
worn cells covered with pores; a raised protuberance on each side of
the zocecium a little lower than the oral aperture; an avicularium
immediately below the aperture, sometimes turned to the right, some-
times to the left ; immediately below the avicularium there is a deep
depression, and the opening of this depression seen from the interior
is found to be an elongated denticulate pore (see fig. 73). Oral
aperture rounded on the distal edge, straight on the proximal, 0°07
mm. wide.
It will be seen that this resembles the form of M. violacea called
330 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
plagiopora, from the Crag, but differs in having an elongate pore;
Escharipora trifora, Roem., from Sollingen, belongs to one of these
forms. The old basal cells, where the oral aperture is obliterated,
show a central depression for the pore and avicularium; and the
whole cell stands out in a mamillated manner.
I have one specimen in which all the zoccia are very much
swollen on one side without any protuberance on the other; and
in the same specimen, at the lower part of the avicularium, there are
three openings, by which the mandible was probably attached.
Loc. Specimen in the Geol. Soc. coll. from Mount Gambier: but
from this alone the detail could not have been worked out. Living:
Indian Ocean (Z.). |
32. MIcROPORELLA FERREA, sp. nov. Plate XVII. fig. 72.
Zoarium erect, in Hschara-form, compressed, few cells. Zocecia
indistinct, slightly raised round the oral aperture, depressed towards
the centre, with a median pore. Oral aperture rounded on the distal
edge, contracted towards the proximal edge, which is straight, thus
having the shape of a circle with the lower third cut off. Small,
erect, oral avicularia in the aperture, in one row on the right, in the
next on the left; small avicularia and large pores round the raised
portion surrounding the aperture; large zocecial avicularia on the
side of the zoarium, with the opening. looking downwards. Oral —
aperture 0-14 mm. at proximal edge, 0: 1S at widest part, 0-14 mm.
long.
The large avicularium was (by an ucbeialte not figured ; but the
beak is about as large as an ordinary zocecium, and it is just the
same in form as the avicularia of Cellaria ovicellosa, fig. 62.
This would be Diporula of Hincks ; but as I am doubtful about
the necessity for the genus, I at present at any rate do not separate
it from Microporella. A reference to my paper ‘‘ On the Use of the
Opercula in the Determination of the Cheilostomatous Bryozoa,” Proce.
Manch. Lit. and Phil. Soc. vol. xvi. no. 2, pl. i. fig. 28, will show
that, in the form of the operculum, Microporella (Diporula) verrucosa,
Peach, is very similar to the present species.
Loc. Fossil: Mount Gambier (Lond. Geel. Soc. coll. 1
33. MicroporELLA ELEVATA, T. Woods. Plate XVIL.: figs. 63, 64;
Plate XVIII. fig. 90.
Eschara elevata, T. Woods, “ On some Tert. Austr. Bry.,” Tr. Roy.
Soc. N. 8. Wales, 1876, De Bo tates, IND).
Zoarium in Eschara- form, foliaceous, compressed. Zocecia, in
young cells (fig. 90), widely oblong to square, with a large short
triangular avicularium pointing inwards on one side of the zoce-
cium on a level with the aperture, or frequently one such ayicula-
rium on each side; in the old cells the zocecia are indistinct, with a
much raised peristome giving a crateriform appearance ; the general
surface and the peristome divided by raised lines into angular areas,
with one or two pores in each such area ; below the aperture a large
pore, which, however, is not always readily distinguished on the front
of the zocecium ; but when examined from the interior (fig. 64) the
ee
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 331
round pore is always seen. Aperture of peristome round; oral aper-
ture, as seen from inside, apparently with a straight proximal edge.
The right-hand side of fig. 63 is the lower part of the zoarium,
being placed sideways to show the structure better. Itis difficult to
decide if this should be placed with Microporella or Porina.
Loc. Fossil: Mount Gambier (Lond. Geol. Soc. coll.).
34, MicRoPORELLA YARRAENSIS, sp. nov. Plate XV. figs. 27, 28.
Zoarium in Hschara-form, subcylindrical, compressed ; branches
dividing dichotomously. Zocecium distinctly bordered, irregularly
oval; peristome slightly raised. Oral aperture round on the distal
edge, straight on the proximal; two large pores immediately below
the aperture; the upper part of the zocecium, supporting the aper-
ture, together with these pores, is raised; a large protuberance on
one side of the zocecium, and a smaller one on the other. In the
central portion of the cell a large depressed area with two or three
openings ; below this area a small avicularium. The zocecium is sur-
rounded with an indistinct row of pores. Three distal rosette-plates
(see fig. 28). Oral aperture 9-6 mm. wide.
When the front of the ceil is slightly worn and the aperture
broken down, the aperture and pores together frequently give a
subtriangular form to the resulting opening.
The details could not have been deciphered from the Mount-
Gambier specimen, though when compared with the better-preserved
specimens marked Yarra-Yarra it is seen to correspond in every
particular.
Loc. Mount Gambier (Lond. Geol. Soc. coll.).
35. MicROPORELLA coscINopora, Rss., var. ARMATA, nov. Plate XV.
fig. 25.
This has a large distinct depressed cribriform area, and an avicu-
larium below this area; the protuberances on the side of the zocecia
are wanting; and the surface of the zocecium is flat; the upper part
of the oral area is raised. Aperture 0-1 mm. wide.
In one specimen in Miss Jelly’s collection there are similar small
avicularia scattered irregularly over the surface.
36. MicRoPORELLA ZNIGMATICA, sp. nov. Plate XV. figs. 29, 30.
Zoarium in Eschara-form, composed of two layers back to back,
forming a very thin lamella, which apparently has considerable
extension (as all the pieces are flat and show no signs of branch-
ing). Surface of zocecium very flat, opening of peristome circular ;
opening of oral aperture, as seen from the interior, arched above,
straight below; depression below the aperture, closed by a cribri-
form plate; large and small acute avicularia scattered abundantly
over the surface. Aperture 0-1 mm. wide.
The surface is very flat, and the openings of the oral aperture and
avicularia being often of nearly the same size and irregularly placed,
it is in some places impossible to decipher any structure. But in the
best-developed and best-preserved parts the peristome is seen to be
slightly raised; and at first it seemed that the form of the aperture
333 24 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
indicated Lepraka; but the interior shows that the lower edge of
the operculum was straight, and that it must be placed with Micro-
porella.
37. MicRopoRELLA SYMMETRICA, sp. nov. Plate XVIII. fig. 83.
Zoarium in Hschara-form, foliaceous. Zoccia hexagonally oval,
distinct, with a thin border round the cell, scarcely raised, with few
pores near the edge, raised in the region of the aperture, especially
above the aperture. Two large openings, directed laterally imme-
diately before the aperture ; these are usually raised and form part
of the peristome. An area on the lower part of the cell with stellate
pores arranged in two series of 4 or 5, each regularly opposite to one
another ; sometimes one or two pores between the lateral rows. This
area usually forms a deep depression; but in some cells this is not
the case. Oral aperture semicircular, with straight proximal edge,
0:09 mm. wide, 0:07 mm. long.
In the species we see a marked likeness to MW. yarraensis (fig. 27);
and through these we are able to trace the relationship of this area
from the round pore of M.violacea to the elongate pore of M. violacea,
var. jissa (fig. 26), to the two or three pores of M/. yarraensis, and
the cribriform pores of MW. coscinopora (fig. 25) and M. enigmatica
(figs. 29, 30), and, lastly, to the depressed area of the present species ;
and we seem justified in extending the comparison and comparing
the non-depressed area of the present with that of Cribrillina
terminata (fig. 68), which, in its turn, may be traced to typical
Cribrillina.
38. MicroporeLia ciavata, Stol. Plate XVIII. fig. 84.
Flusirella clavata, Stol. Foss. Bry. Orak. p. 139, pl. xx. figs. 3, 5.
Zoarium in Hschara-form, forming thin foliaceous dichotomous
branches or small round branches. Zocecia suboval, contracted and
truncate below; a characteristic semicircular depression immediately
below the aperture, with three large raised pores, the two upper
ones directed to the right and left. A laterally oval depression or
opening about the middle of the zoccium, with the median pore
~ below this. Oral aperture semicircular, with a straight proximal
edge, 0:07 mm. wide, 0:05 mm. long.
This is much the same as Eschara tetrastoma, Rss. Sitz. Ak. W.
Wien. 1864, p. 9, pl. i. fig. 9.
Loc. Fossil: Orakei Bay.
39. Porina CLYPEATA, sp. nov. Plate XVII. fig. 67.
Zoarium erect, cylindrical ; four zocecia in a complete series, al-
ternating regularly with each other, and facing in four directions.
Zoecia distinct, tubular; peristome much projecting; median pore
placed about one half the length of the cell, opening at the top of a
cone, the base of which is surrounded by an oval or circular rim,
giving it ashield-like appearance. This rim is continued in a straight
line above and below. A small obtuse avicularium on each side of
the shield-like boss.
a a oe
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA, S53)
This is a very interesting specimen, as the shield-like elevation
gives ita peculiar appearance different from any thing with which we
are acquainted ; and at first I did not know in what way the struc-
ture must be interpreted, and examined to see if it could be an ovi-
cell, but think it must be considered homologous with the tubular
pore of P. tubulosa. The specimens are all small.
Loc. Fossil: Mount Gambier (Zth., jun., coll.).
40. Portna coronata, Rss. Plate XV. fig. 57.
Cellaria coronata, Rss. Foss. Polyp. des Wien. Tert. p. 62, pl. viil.
fig. 3.
Eschara conferta, Rss. loc. cit. p. 71, pl. vii. fig. 32.
Acropora coronata, Rss. Foss. Anth. & Bry. d. S. von Crosaro ;
Denk. math.-nat. Cl. k. Akad. der Wissensch. Wien, vol. xxix. 1868,
p. 65, pl. xxxiv. figs. 33-55.
Spiroporina vertebralis, Stoliczka, Foss. Bry. Orak. p. 106, pl.
xvii. figs. 6, 7.
Spiroporina veriebralis, T. Wocds, ‘‘ Corals & Bryozoa of Neozoic
Period in New Zealand,” Pal. of New Zeal. pt. iv. Colon. Mus. &
Geol. Survey Dept. 1880, p. 23.
Porina Dieffenbachiana, Stoliczka, loc. cit. p. 135, pl. xix. fig. 20.
Porina Dieffenbachiana, 'T. Woods, “C. & Bry. of Neoz.” loc. cit.
p. 25.
Eschara Buskii, T. Woods, ‘On some Tert. Austr. Polyz.,” Tr.
R. Soc. N.S. Wales, 1876, p. 149, figs. xvi. & xvii.
Myriozoum australiense, Haswell, “On some Polyzoa from the
Queenland Coast,” Proc. Linn. Soc. N. 8S. Wales, vol. v. pt. 1, 1880,
p. 43, pl. iii. figs. 9-11.
This species has caused me much trouble, as its appearance in
various conditions is very different ; but direct comparison of typical
specimens with Acropora coronata from Val di Lonte showed that
the size, form of the cell, peristome, median pore, and small pore
were sometimes just the same.
The zoarium is sometimes round and very slender, asin fig. 57; in
others round and stout, as in Stoliczka’s figure of S. vertebralis ; but
having a complete intermediate series, there is no doubt that they
must be united. In other specimens, especially those from Mount
Gambier, the branches are flattened as in P. Dueffenbachiana,
Stol., fig. 20. The surface sometimes has small elongate pores,
in other cases larger and round ones. In theslender specimens the
pores are finer and more elongate, while in the stoutest they corre-
spond with the pores of the Italian P. coronata. Again, the
peristome in young cells is very thin and projects considerably ;
while in older specimens the large pores in the walls of the peri-
stome are more distinctly seen; and in very well preserved speci-
mens the walls of these project, so that each peristomial pore may
be said to have itself a peristome. The median pore is usually about
one quarter of the length of the zocecium from the oral aperture, but
sometimes much nearer ; and in old cells, where the peristomial wall
is much thickened, it approaches very close to the peristome, and
oot A. W. WATERS ON FOSSIL CHILOSTOMATOUS
almost becomes part of the peristomial crown. Ihave only one or
two specimens in which there is a slightly projecting tube for this
median pore ; and in all other cases it is depressed. In some spe-
cimens, besides the small surface-pores, there are larger ones, which
have in most cases been avicularia; and in a few specimens there is
a larger spatulate avicularium above the oral aperture.
In a recent specimen in the vertebralis condition, from Darnley
Island, I found that a section made from one end showed the central
spongy structure with which we are acquainted in the old genus
Myriozoum, while a section made from the other showed the cells
ranged round the circumference but not meeting in the centre:
and a section is thus figured by Mr. Haswell (doe. cit. fig. 10).
Stoliczka, in his figure, distinctly showed this Myriozoum character ;
and it is strange to find that he nevertheless placed the species
among the Cyclostomata. The slender forms so nearly correspond
with Porina borealis, Busk (especially as figured by Smitt in his
‘Floridan Bryozoa,’ pl. vi. fig. 144), that, if not the same, they are
closely related to it; and the species is also related to Porima
filograna, Goldf., figured in d’Orb. Pal. Frang. pl. 626. figs. 5-10, a
common species in the Senonian, and also figured by Hagenow as
schara Defrancei. Several of Hagenow’s species with other names
may represent worn specimens, as pointed out by d’Orbigny.
Although the different conditions pass so gradually from one to
another that it is impossible to separate them, it may perhaps be
useful to speak of them as condition (a) slender, as fig. 57 ; (6) stout,
as vertebrals, figured by Stol.; (c) more flattened, and showing the
quincuncial arrangement more clearly, as in Dieffenbachiana.
Loc. Fossil: Bartonian, Val di Lonte (Ztss.), Montecchio Mag-
giore (ftss.), Vienna (fss.); Ferrara di Monte Baldo, Crosaro, Bren-
dola (all in my coll.); Hutchinson’s Quarry and Oamaru, New Zea-
land, in Lower Eocene of New-Zealand geologists (as ¢, Woods);
Hutchinson’s Quarry, Upper Eocene ditto ; Shakespeare Cliff, Upper
Miocene ditto (as 6); Orakei Bay, New Zealand (6 & ¢, Siol.);
Mount Gambier (Woods, 6 & c); and common in the Lond. Geol.
Soc. coll., and also Eth., junr., coll. from Mount Gambier (as 6).
Living: as 6, Holborn Island, Queensland, 20 fathoms (Hasw.),
and Darnley Island, Torres Strait, in material sent me by Mr. Brazier,
from soundings in 10-30 fathoms.
4]. Pormya? cotumnata, sp. nov. Plate XVIII. fig. 88.
Zoarium cylindrical, erect, with six cells in a complete series, con-
sisting of two rows of three each. Zocecia irregularly oblong, with
nearly parallel sides, distinct, separated by a wide rounded ridge,
surface rounded, with much-raised acute granulations ; the peristome
forms a closed arch over the lower part of the oral aperture ; the
opening at the base of this arch is wide and laterally oval; a large
tubular avicularium on each side of the peristome, also raised and
_ continuous with the peristome. Oral aperture rounded below, pro-
bably round to saddle-shaped, somewhat contracted above. '
The specimen is in a bad state of preservation; and diagnosis
a
a_i
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 335
has to be made from the characters in various cells ; consequently
the figure is, to a large extent, a restoration, which is not the case
with the other figures. I have shown the effect when the aperture
is broken down in different degrees: when completely worn away,
three nearly equal openings are seen, the central one being some-
what the largest ; in other cases an elongate opening is formed,
bounded on the top by the distal end of the peristome, and below by
the base of the subperistomial opening.
This is closely related to Eschara heterostoma, Reuss (Bry. von
Crosaro, p. =°7,, pl. xxvi. fig. 5), which we believe is synonymous
with his #. duplicata (loc. cit. p. (61 sep.) 273, pl. xxxiii. figs. 8,
10), from the Italian Eocene.
The shape of the oral aperture would seem to be Lepralian, perhaps
much the same as in Lepralia Pallasiana ; and itis somewhat a matter
of doubt where this form should be generically placed. There are
some species as yet undescribed from the southern hemisphere, with
an arch more or less enclosing the aperture; and until these have
been examined, it must be placed with Porina.
Since the above was written, Mr. 8. O. Ridley has published, in
the Proc. Zool. Soc. 1881, an “ Account of the Zoological Collection
made during the Survey of H.M.S. ‘Alert’ (pt. Polyzoa),” and de-
scribes and figures an incrusting species with cells much. resembling
those of P. columnata. For this he forms the genus Gigantopora,
and points out the similarity to Hippothoa fenestrata, Sm., which
seems to sometimes occur in an erect form; and these three spe-
cies are evidently closely related ; but we provisionally retain the pre-
sent one under Porina until more complete specimens furnish further
characters upon which the genus can be founded.
42. LEPRALIA CORRUGATA, sp.nov. Plate XVII. fig. 60.
Zocecia elongate, distinct, raised ; surface in irregular ridges and
furrows; in the furrows a row of one or two pores; lower part of
zocecia depressed, upper raised, with a large angular avicularium
forming a kind of peristome over the lower part of the aperture ;
one or two large pores at the lower part of the zocecium, just above
the aperture of the zocecium next below. Aperture rounded. Zoa-
rium either incrusting or in Hschara-form.
Oral aperture 0°14 mm. wide.
43, LEPRALIA MONILIFERA, M.Ed., var. arMATA. Plate XV. fig. 24.
Zocecia elongate, pyriform, raised in the centre, with a row of
pores round the border ; aperture oval, proximal edge slightly less
rounded than the distal; a small angular avicularium on one or
both sides of the aperture; in some cells larger angular avicularia
below the aperture.
Aperture 0-11 mm. wide; 0:14 mm. long.
Only a small fragment, worn at the back.
44, LEPRALIA SPATULATA, sp.nov. Plate XVIII. fig. 87.
Zoarium erect, forming a solid stem, with zocecia all round.
336 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
Zoecia hexagonal, distinct, with a thin border slightly rounded,
raised towards the aperture; surface finely granular; the region
above the aperture is much raised, with six spines, three on each
side. Aperture nearly circular, slightly elongate, situated in a wide
depression, caused by the elevation round the sides and distal part
of the aperture. Aperture 0°15 mm. wide, 0°17 long.
This much resembles Lepraha multispmata, Busk, from Madeira
(Q. J. Micr. Sc. new ser. vol. i. 1861, p. 78, pl. xxxii. fig. 5); but
the lip below the aperture is entirely wanting.
In a specimen from the Mount-Gambier collection of Mr. Ethe-
ridge, jun., there are many large spatulate zocecial avicularia scat-
tered over the stem.
Loc. Fossil: Mount Gambier.
45, LEPRALIA CLEIDosToMA, Sm., var. roTuNDA. Plate XVIIL. fig. 92.
Zoarium apparently flat and incrusting. Zocecia small, distinct,
hexagonal ; surface coarsely granular. Oral aperture orbicular, con-
tracted at the sides by two denticles; raised rounded avicularium
(perhaps with vibracular characters) below the line of the aperture,
on the side of the zocecium ; four lateral rosette-plates, one distal near
the base of the zocecia. Oral aperture 0°1 mm. wide, 0°13 long.
It is difficult to know where this should generically be placed.
From the rounded distal and proximal edges of the aperture, it would
have gone with Smitt’s earlier definition of Escharella. In the size
and form of the cells it much resembles Schizoporella excubans, fig. 56;
but this, instead of being an erect quadrilateral form, is incrusting,
and has a rounded avicularium ; but we may perhaps here trace the
passage from a definite sinus to a rounded proximal edge. It only
differs from Lepralia cleidostoma, Smitt (Flor. Bry. p. 62, pl. xi.
figs. 217-219), in having the rounded avicularium instead of an acute
one, and should, perhaps, be united to it.
I have an erect branching form, with ovicells, from the Mediter-
ranean, Closely allied to this, which I hope shortly to describe and
figure.
Mr. Hincks has kindly informed me (in htt. ee that he has this va-
riety from Bass’s Straits.
46. PoRELLA EMENDATA, sp. nov. Plate XVII. fig. 69.
Zoarium in Eschara-form.
Surface nearly flat; cell-wall thickened round the oral aperture.
Zocecia elongate, expanded above, contracted below; row of pores
in a furrow on each side of the zoccium. Aperture round on the
distal edge, straight on the proximal, with a very large denticle
set deeply in the aperture. Small triangular avicularium below
the mouth, usually placed somewhat diagonally.
Aperture on proximal edge 0:07 millim. wide, 0-06 millim. long.
47. PoRELLA DENTICULATA, Stol. Plate XVII. fig. 70.
_Plustrella denticulata, Stoliczka, Foss. Bry. Orak. p. 138, pl. xx.
fig. 2.
Oral aperture arched above, contracted below, enclosing an ayicu-
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 307
larium surmounted by a denticle ; faint lines on the surface indicate
the zocecial divisions. Ovicell subimmersed, without any pores.
Loc. Not very common in Orakei Bay.
48. SMITTIA CENTRALIS, sp. nov.
Zoarium slender, erect, quadrangular, with the zocecia on all four
faces. Zocecia separated by a ridge, elongate, oblong, flat, with a
double row of pores on both sides of the zocecia near the edge,
with the peristome very much raised and projecting, with a large
pore (probably avicularian) immediately below the or ifice ; SER DET
transversely oval.
49. SMITTIA CENTRALIS, var. LHVIGATA. Plate XIV. figs. 7, 8.
Differs from the above in haying the surface of the zocecia slightly
rounded ; and instead of the two rows of small pores, there are
a few elongate pores near the edge of the zoccia; the peristome is
less well preserved ; and from these small fragments it would be
impossible to be sure of the generic position of the species. The
distal rosette-plates (fig. 8) are near the centre of the zoarium, from
which circumstance the name is chosen.
50. Smirrra Tarrr, T. Woods. Plate XVII. fig. 65
Eschara Tatei, T. Woods, “ On some Tert. Austr. Fossils,” Tr. R.
Soc. N.S. W. 1876, p. 3, fig. xv.
Zoccia elongate, with parallel sides, contracted below, surrounded
by a narrow raised margin ; two perforated furrows down the front.
Aperture raised, rounded, with a second rounded opening imme-
diately below (this is probably avicularian). Seen from the inte-
rior, there is a large denticle expanded at the top (fig. 65 a).
Aperture 0°13 millim. wide.
In consequence of the imperfect state of fossilization of the Mount-
Gambier fossils, the aperture presents the appearances figured by
Mr. Woods. A specimen in the collection of Mr. Etheridge, jun.,
shows cells as figured by Mr. Woods, and resembling those from the
present collection.
Loc. Fossil: Mount Gambier (Woods and collection of Mr. Ethe-
ridge, jun.).
51. Surrrra anceps, MacG. Plate XVIII. fig. 94.
Lepralia anceps, MacGillivray, Prodr. of Zool. of Vict. decade iv.
e7sp. 20, pl. xxxv. fig. 6.
Zoarium cylindrical; in one specimen four or five cells in a series,
in another a hollow cylinder 2-5 millim. in diameter. Zocecia sub-
rhomboidal, sometimes hollowed in front, elevated towards the ori-
fice, bounded by a prominent irregular sinuous line; surface very
finely granulated, with large pores, more numerous near the edge.
Oral aperture rounded on the distal end; the proximal edge is
formed by the arc of a smaller circle.
When the aperture is seen from inside, we find a broad denticle
(fig. 94a); and when we look upon this denticle from above, it is
Pate) A. W. WATERS ON FOSSIL CHILOSTOMATOUS
seen to bear avery minute avicularium. Aperture 0-1 millim. wide,
0°14 millim. long. |
‘If I had been unable to see the interior of the zocecium, I should
have considered this to be Schizoporella sinwosa, B., with which it
corresponds in most particulars. I have examined the interior of
S. stnuosa from Shetland, in which there is no similar denticle or
avicularium. Some of the zocecial areas have no aperture; and m
' these there are few or no pores.
52. ScHIZOPORELLA VIGILANS, sp. nov. Plate XIV. fig. 13.
Zoarium erect, quadrilateral, with zocecia on the four faces. Zooscia
irregularly oblong; surface flat, with elongated pores (reminding us
of those of Hornera); upper part of the zocecium slightly raised.
Oral aperture rounded on the distal edge, nearly straight on the
proximal, with a well-marked sinus. Acute avicularia, placed hori-
zontally in the middle of the front wall of the zocecium.
The proximal edge of the oral aperture is slightly straighter than
figured. Aperture 0:08 millim. wide, 0:07 millim. long.
53. SCHIZOPORELLA PHYMATOPORA, Rss. Plate XV. figs. 31, 32.
Eschara phymatopora, Reuss. ‘ Foss. Anth. u. Bry. von Crosaro,”
Denschr. Ak. Naturwissensch. Wien, vol. xxix. 1869, p. 272 (60),
jl soroxibbly 11k 1p |
Zoarium cylindrical. Zocecia irregularly oval, not much raised ;
border distinct. Aperture circular, with sinus below. Avicularia
at about one third or the middle of the length of the zocecium, placed
on one side; surface of zocecium covered with pores and fine gra-
nulations.
When I drew fig. 32, I supposed that this was Bactridiuwm, and
allied to Bactridium Hagenowi, Rss.; and then I called it tr-
serrata, aS in all the fragments I had there were three rows of
cells. Since then fragments in my own and in Miss Jelly’s
collection have shown that it is cylindrical. The species splits
up with considerable regularity ; and then the other sides of the
zocecia are seen with their lateral rosette-plates appearing like a row
of pores. A central furrow is also seen with two rosette-plates for
the entrance of the endosarc. The avicularia are usually much
lower than figured by Reuss in his specimen from the Val di Lonte,
but in some Australian specimens are higher than in my figure 31.
Aperture 0:07 millim. wide.
Loc. Val di Lonte (#ss.); Ferrara di Monte Baldo (A. W. W.):
Bartonian.
54, ScuizopoRELLA VENTRICOsA ?, Haswell (in Onchopore forma).
Onchopora ventricosa, Haswell, “On some Polyzoa from the
Queensland coast,” Proc. Linn. Soc. N. S. Wales, vol. v. pt. i. 1880,
p. 36, pl. 1. fig. 3. ;
There is only a small fragment, which has the zoarium cylindrical,
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 309
and which seems to branch without joints. It seems to correspond
with the above ; but there is reason for doubting whether too many
species have not been made, as Onchopora ventricosa, Hasw., and 0.
granulosa, H., are very closely allied.
Loc. Holborn Island, Queensland, 20 fathoms.
55. ScHIZOPORELLA FENESTRATA, sp. nov.
Zoarium in Kschara-form. Zoccia indistinct, surface smooth.
Oral aperture very large, in a very deep depression, rounded on the
distal edge, with a sinus on the proximal; a small rounded avicularium
within the oral depression, and a small rounded one below the aper-
ture with avicularium opening with numerous denticles. Very large,
erect, angular avicularium between the zoccia. Oral aperture 0°17
millim. wide.
The large deep depressions round ie large aperture, together with
the smooth surface and small avicularia, gives the zoarium the ap-
pearance of the network of Retepora; and the specimen was sent to
me marked Retepora. I therefore call it fenestrata, although, of
course, it is clear that itis here the magnified aperture which repre-
sents in appearance the unmagnified fenestra of Retepora.
56. ScHIZOPORELLA, sp.
Zocecia perfectly parallel, oblong, distinctly divided laterally, ter-
minal divisions scarcely distinguishable. Surface smooth. Oral
aperture large, 0°3 millim. long, 0°22 millim. wide, rounded above,
apparently triangular below ; frequently a notch on one side, as
if regularly broken down; perhaps there is an avicularium inside
the aperture below the notch. ‘The back of the cells is also smooth,
showing the lateral parallel divisions distinctly, with an oval open-
ing 0:4 millim. long, 2. ¢. about half the length of each zocecium.
There are one or two species in which there is a similar oval
opening on the dorsal surface; but at the»present moment I do not
find any note or reference to such, except in Hemeschara gemi-
nupora, Rss.
57, SCHIZOPORELLA, SP.
This somewhat resembles S. biaperta; but the state of preserva-
tion is not sufficiently satisfactory for definite determination. The
aperture is much smaller than in the last species; and there are
numerous round avicularia scattered over the cell. The walls of
the ovicells, which have been considerably raised, are broken down.
This may be Hscharipora Lawderiana, Stol. (Bry. Orak. Bay, p. 136,
pl. xx. fig. 1); but the figure and description are so unsatisfac-
tory that it is impossible to know where Stoliczka’s specimen
should be placed. The fossil specimen is in the Aschara-form.
A specimen in the British Museum, sent by Mr. Hutton, marked
Lepralia reticulata, seems to be this species. The oral aperture of
the recent specimen is rounded on the distal end, with a smaller arc
forming a sinus on the proximal. |
340 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
58. ScHIzoPoRELLA SUBMERSA, sp. nov. Plate XVIII. fig. 85.
Zoarium in Hschara-form, consisting of narrow foliations. Zo-
cecia suboval, expanded above, contracted below, distinct, sur-
rounded by a raised border, partially concave, few pores on the sur-
face. Acute avicularium near the centre of the zocecium, sometimes
directed diagonally upwards, sometimes downwards. Oral aper-
ture very long, rounded on the distal end, with a small sinus on
the proximal. ‘The aperture is much depressed, giving the ap-
pearance of two wide denticles at the bottom of the oral pit. Aper-
ture 0-07 millim. wide, 0°12 millim. long (to end of the sinus).
The upper part of the zoceclum being depressed gives a concave
appearance to the zocecia.
59. ScHIZOPORELLA CONSERVATA, sp. nov. Plate XVIII. fig. 81.
Zocecia suboval to oblong, distinct, not much raised, sometimes
with a median raised ridge extending from the sinus; a few large
pores near the edge; surface smooth; three spines above the oral
aperture, and one on each side at the base of the aperture; surface
slightly raised below the sinus. Oral aperture semicircular, rounded
on the distal edge, straight on the proximal, with a small sinus
which widens out below. An avicularium on one or both sides a
short distance below the oral aperture; these vary from short
triangular to acute lanceolate, pointing laterally outwards at right
angles to the axis of the cell. Ovicells very large, elevated, with
the central part plain, and nearly flat, the exterior walls beautifully
ornamented with radiating lines with three pores between each.
Aperture 0°16 millim. wide, 0°12' millim. long (to the straight
proximal edge). |
When the avicularia are small, they are raised ; but when large,
they are immersed. The dorsal surface is hexagonally divided, with
an elongate oval space (about half the length of each zocecium) of
thinner shell. This perhaps corresponds with the “ flattened disk ”
mentioned by Mr. Busk in Microporella Malusw, Aud. (Mar. Poly.
p. 83); but it is by no means a constant character in Malusi, as
the centre of the dorsal surface is usually depressed, with irre-
gular elevations near the edge of the zoccium. The structure of
the dorsal surface of Schizoporella conservata must probably be com-
pared with that of Schizoporella, sp., No. 56. I presume this spe-
cies grew in the Lepralia-form.
Loc. Fossil: Mount Gambier (Lond. Geol. Soc. coll. and Eth.,
Jun., coll.).
60. ScHIZOPORELLA SPIROPORINA, Sp. NOv.
Zoarium cylindrical ; zocecia in annular series of six cells; series
0-7 millim. apart. Zocecia indistinct, except towards the peristome ;
_ peristome much raised in front, but very little behind. Oral aper-
ture at the base of the peristome, nearly circular, rounded at the
distal end, with a widesinus at the proximal. Large pores, perhaps
avicularian, near the peristome.
This may be Spiroporina immersa of T. Woods (Corals & Bry. Col.
BRYOZOA FROM §.W. VICTORIA, AUSTRALIA. 541
Mus. & Geol. Survey New Zealand, pt. iv. p. 23); but I must con-
fess to being unable to understand Mr. Woods’s description of the
mouth. The specimen from ‘ Yarra-Yarra” is very small and in
imperfect preservation.
61. ScHIZOPORELLA EXCUBANS, sp. nov. Plate XVI. fig. 56; Plate
XVIII. fig. 80.
Zearium erect, filiform, with a longitudinal row of zocecia on each
of the four faces. Zocecia distinct, subhexagonal, upper part much
raised, surface granular. Oral aperture depressed, rounded on the
distal] edge, contracted on each side near the proximal edge, forming
a large rounded proximal sinus. Triangular avicularium on raised
prominence on a level with the oral aperture, directed downwards.
Avicularia sometimes absent, usually on one side only.
Aperture 0-08 millim. wide, 0-075 millim. long.
Probably the genus Schizoporella will have to be broken up, and
those forms in which the proximal edge of the oral aperture forms a
large arc will be separated; for while the appearance is that of a
large sinus, the structure must be different. It is also very diffi-
eult to see where the division should be made between Lepralia and
Schizoporella ; for the wide rounded aperture of Lepralia with two
lateral denticles sometimes approaches very closely in shape that of
a Schizoporella with a large and wide sinus. Fig. 56 was drawn
from a small fragment in which it was impossible to see the form
of the zoarium, and therefore, in this respect, is not quite correct.
I have since received specimens showing the erect filiform growth.
62. ScHIzoPORELLA AMPHORA, Sp. Nov.
Zoarium slender, erect, with a single row of zocecia on each of the
four faces, the opposite pairs alternating with the othertwo. Zocecia
irregularly ovate, expanded _and raised in the middle, contracted above
and below ; distal end of the zocecium much raised, forming a small
peristome which is contracted on both sides near the lower part.
The specimen is small; and more perfect ones may add many
particulars. It may have been sometimes articulated, as seems to
have been the case with Cellaria Schreibersi, Rss.
63. ScHIZOPORELLA AUSTRALIS, T. Woods. Plate XIV. fig. 15.
Tetraplaria australis, T. Woods, “On some Austr. Tert. Foss.
Corals & Polyzoa,” Tr. Roy. Soc. of New 8. Wales, 1878, p. 5, fig. 4.
Zoarium cylindrical, slender. Zocecia facing four ways, the op-
posite pairs alternating with the other two, elongately pyriform ;
surface very finely granulated, with extremely fine pores between
the granules (but these can only be seen when the preservation is
very good). Oral aperture rounded on the distal edge, slightly curved
or straight on the proximal, with a small distinct sinus; aperture
0-08 millim. wide, 0°07 millim. long.
Since I drew the figure I have received a much better specimen,
from which J have been able to make out the character of the
aperture. The cells are nearly half as long again as in Cellaria
Q.J.G.8. No. 147. 2A
342 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
Schreibersi, Rss., with which Mr, Woods compares it; and, further,
the two prominent avicularia are wanting; but from my Val-di-
Lonte specimens of C. Schretbersi I find that both belong to the Schi-
zoporellidse, and are allied in many particulars.
Loc. Muddy creek, Western Victoria ( W.).
64. Rerepora marsupraTa, Smitt. Plate XV. figs. 34, 35, 36;
Plate XVII. figs. 59, 61, 76, 77.
Retepora marsuprata, Sm. Floridan Bry. p. 67, pl. xiii. figs. 245-
254; Svenska Vetensk. Handlingar, vol. xi. 1872.
Phidolophora labiata, Gabb & Horn, ‘“* Polyzoa of Second. and Tert.
Form. of N. Amer.” p. 138, pl. xix. fig. 21°(Journ. Ac. Nat. Sei.
Philad. vol. v. pt. i1.).
Zoarium reticulate. Zocecia suboval to hexagonal, separated by
a distinct raised border; peristome elevated in young cells; in old
ones the aperture is immersed, with sometimes a spine on each side
of the aperture; in front of the peristome a ridge, at the base of
which is sometimes a small pore (sometimes avicularian); this gives
a distinctly sinuated appearance to the peristome: in some speci-
mens large, erect, angular avicularia in the middle of the zocecium ;
in others large erect more spathulate avicularia; in others very long
and very narrow immersed ayicularia in a similar position, with the
mandible in all cases pointing directly or diagonally downwards ;
sometimes there are small rounded avicularia pointing downwards,
with a central pore. Surface smooth, or with few granulations ; often
two large pores near the proximal extremity of the zoccia. One
ovicell is subimmersed, with one cleft, as described by Smitt ; ano-
ther is more raised and more globose, with two depressed lines close
together instead of the one central cleft; and there is also a small
boss on the centre of the ovicell. The dorsal surface, which is
divided irregularly by thin raised lines, has minute rounded avicu-
laria scattered about; there are also long, triangular, immersed
avicularia and large erect ones. In the basal portion the aperture
is depressed, when we find the structure figured in figs. 59, 61,
and 76, which are drawn from different specimens ; but interme-
diate ones leave little doubt as to their identity.
In these we see the median pore representing avicularia, and
showing the relationship to Portna. Median pores are known in
Retcpora tuberculata, Rss. Some of the basal branches seem to show
that reticulation was much less frequent than in most Retepore ; and
this and &. rimata would be Psilescharew of Busk, a genus which
cannot be retained. ’ :
It is impossible to be quite sure if this is the same as the fossil
described by Gabb and Horn. It is evidently allied to R. Beanzana,
King, and probably is the species described under that name by
Stoliczka. The suboral pore represents the suboral avicularium in &.
Beaniana; and small avicularia are found on the front of Beanana.
Loc. Living: Floridan seas, 16-262 fathoms (Sm.); Teneriffe
(Busk). Fossil: Miocene, 8. Barbara, Amer. (G. & H.); Mount
Gambier (Lond. Geol. Soc. coll.).
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 343
65. Rerepora rmmata, sp. nov. Plate XVI. figs. 48, 53.
Zoarium probably reticulate; branches slightly compressed.
Zocecia cylindrical, convex ; surface smooth ; peristome much raised,
with a cleft in front the whole length of the peristome, expand-
ing at the base, the edges on the two sides of the cleft turned
inwards, peristome often surrounded in front with a raised rim.
Small subimmersed avicularia below the peristome, subtriangular
or suboval, pointing upwards, with a very minute opening near the
distal end. Dorsal surface divided by white raised lines, with small,
subcircular, acute avicularia and small bosses irregularly placed.
This is common from Mount Gambier; but the state of fossi-
lization would not have permitted all the characters to be made
out if the “ Yarra- Yarra” specimens had not served as a key.
Loc. Fossil: Mt. Gambier (Lond. Geol. Soc. and Hth., jun., coll.).
In one specimen the avicularia in the front are replaced by asimple
pore. This would unite the genus with Porinide; and we here see
another example of the avicularia taking the position of pores, and
are led to regard avicularia as modified pores.
66. CELLEPORA YARRAENSIS, Sp. NOV.
Zoarium cylindrical, dividing dichotomously, in one case throwing
out a branch forming an angle of about 80°; diameter of stem 1-2
millim. Zocecia very irregularly arranged, placed sometimes very .
crowded, sometimes far apart, indistinct ; peristome much raised on
the lower or avicularium side, usually not at all on the other, giving
it, when seen in profile, a triangular appearance; at the proximal
part of the peristome an avicularium ; when this is broken down the
two large openings have the appearance so general in Cellepore ;
between the zocecia few large much raised perforated protuberances,
probably sometimes avicularian. Surface smooth, porcellaneous.
Oral aperture semicircular, rounded on the distal edge, straight on the
proximal, though when raised cells are seen the aperture appears
rounded. Aperture 0-08 millim. wide, 0:1 millim. long.
I have an undescribed thin branching species of Cellepora from
Capri (near Naples) which also has the lower edge of the aperture
straight and in many respects resembles the present.
67. Ce~tepora Fossa, Hasw. Plate XVIII. fig. 89.
Spheropora fossa, Haswell, “ On some Polyzoa from the Queens-
land Coast,” Proc. Linn. Soc. New 8. Wales, vol. v. pt. i. 1880, p.
42, pl. ii. fig. 5, 6.
Zoarium subglobular, flattened above, specimens 2—5 millim. in
diameter. On the upperside the zocecia are directed from the pole of
the zoarium ; on the underside they are directed towards it. Zocecia
subcylindrical or ovate or conical, very finely granular, erect (on
the upperside) ; a few pores round the edge of the zoecium on the
' upperside, but seldom on the back. Oral aperture rounded on the
- distal wall, straight on the proximal. In the centre, immediately
below the proximal margin, a large, wide, erect, obtusely conical or
globular avicularium. Few large, spatulate, zocecial avicularia
Za 2
o44 - A. W. WATERS ON FOSSIL CHILOSTOMATOUS
scattered over the colony. Aperture 0:12 millim. wide, 0:1 millim.
long.
I cannot attach any importance to the pit round which the zocecia
are formed and upon which Mr. Haswell’s new genus is founded.
The form of the oral aperture is rare in the Celleporide ; but we see
the same thing in C. sardonica, Waters (“ Bry. Bay of Naples,” Ann.
Nat. Hist. 1879, p. 196), also in C. yarraensis, W., in C. intermedra,
M‘G., and in C. compressa, Busk, with which perhaps the above
should be united; and perhaps these together should form a sub-
genus. This may be one of the Cellepore described by Mr. Tenison
Woods in “ Tertiary Fossils in S. Australia,” p. 5 (Trans. Roy. Soe.
of Victoria, vol. vi.); but identification with these is impossible, as
the zoarial instead of the zocecial characters are described. In de-
scribing fossil Bryozoa so little attention has been paid to the most
important character, 2.¢. the form of the oral aperture, that com-
parison is often not possible.
Loe. Living: Holborn Island, Queensland, 20 fathoms. Fossil :
Mount Gambier (Lond. Geol. Soc. and Hth., jun., coll.).
68. CELLEPORA, sp.
There are a few cells of a Cellepora which resemble those of
C. pumicosa, Busk (non Linn.); but the fragment is too small to
determine with certainty.
69. LUNULITES GUINEENSIS, Busk. .
Cupularia guineensis, Busk, Cat. Mar. Polyz. p. 98, pl. exiv.
The specimen in Miss Jelly’s collection is very small; but as the
few zocecia correspond in shape with those figured by Mr. Busk,
we may safely conclude that the same species is ; represented.
Loc. New Guinea (B). .
70. LUNULITES CANCELLATA, Busk.
Lunulites cancellata, Busk, Cat. Mar. Pol. p. 101, pl. exiii. figs. 4-7.
Loc. Philippine Islands (Busk); off Raton, New Guinea, 7
fathoms, and from Darnley Islands, Torres Straits, 10-30 fathoms
(sent me by Mr. Brazier).
71. Sevenarza MaRGINATA, T. Woods. Plate XVII. fig. 71.
Selenaria marginata, T. Woods, “On some recent and fossil
Species of Australian Selenariade (Polyzoa),” Trans. Phil. Soc.
Adelaide, 1880, p. 9, pl. i1. fig. 9, a—d.
The zocecial cells are very small, and in shape resemble those
drawn by Mr. Woods. In some of the zocecia there is a plate, some
little distance down the aperture, with a central perforation, so that
the zocecium is almost closed. Sometimes the same thing is seen in
Cellaria fistulosa both recent and fossil. I hardly understand
Mr. Woods’s description or plate when he refers to the pore; but I
think this is undoubtedly the species he describes. Aperture 0-06
millim. wide.
Loe. Living: Cape Three Points, 71 fathoms.
BRYOZOA FROM S.W. VICTORIA, AUSTRALIA. 345
72. Sermnapgia ALATA, T. Woods.
Selenaria alata, Tenison Woods, “On some recent and fossil
Species of Australian Selenariade (Polyzoa),” Trans. Phil. Soc.
Adelaide, 1880, p. 11, pl. u1. fig. 12, a, 0, ©.
Loc. Muddy Creek, Miocene Beds near Hamilton, Victoria (W.).
The specimen is smaller than those described by Mr. Woods,
only measuring 23 millim.; but otherwise the differences are very
small and do not seem sufficient to make it a variety. The specimen
may be described as follows :—Zoarium small, orbicular, moderately
convex. Zoccia rhomboidal or semicircular, margins distinct ; area
depressed, aperture large, narrowed below by triangular ale at each
side. Avicularian areas few, not so large as the zoccia. Under
surface with radiating grooves.
All Mr. Woods’s figures for the above memoir are lesa upside
down, perhaps by an error of the lithographer; and Mr. Woods
seems to have described his species from the figure when he says of
the aperture “‘ narrowed above ” instead of “ below.”
Besides the specimens determined, there are several imperfect
fragments of other species, among which there is a badly preserved
Lunulites somewhat resembling L. aperta, T. Woods; and there are
a few cells of a species (probably with Lepralia growth) with ven-
tricose punctured cells and a long projecting spout below the aper-
ture resembling that of L. mamillata (Crag Polyz. pl. vi. fig. 5),
and a few zocecia of an erect form with elongate subtubular coarsely
punctured zocecia with a projecting wide peristome ; each zoceclum
- springs laterally from the one below, in the same manner as in C/r7-
brillina dentipora, fig. 33.
EXPLANATION OF PLATES XIV.-XVIII.
Pruate XIV.
Fig. 1. Cellaria fistulosa, L., 2°, showing openings for the horny connecting
tubes.
2 , 22, showing ee and ovicell.
3. —— malvinensis, nice 25, showing avicularia.
4 ovicellosa, Stol.,
5. Section of ditto.
6, Central walls of ditto, showing rosette-plates.
7. Smittia centralis, var. levigata, nov.
8
9
10
12
. Section of ditto, showing eee plates.
. Membranipora maorica, Biol Bs
, Ll. Cellaria fistulosa, Le
. Cellaria sp., 2°
13. Schizoporella vigilans, sp. noy., 25
14, Membranipora lusoria, sp. nov., 2
15, Schizoporella australis, Ate Woods,
16. Cellaria globulosa, sp. nov. 22.
17. End view of do.
18, 19. Membranipora macrostoma, Rss., 32.
20, 21. argus, AOrb., 3,2: a, lateral rosette-plates.
22, 23. concamerata, sp. nov. 332.
346 A. W. WATERS ON FOSSIL CHILOSTOMATOUS
Prare XV.
26. violacea, var. fissa, 25.
27, 28. Microporella yarraensis, sp. nov., 25.
29. Microporella enigmatica, sp. nov., *.
30. , seen from the interior, showing cribriform plate.
31. Schizoporella phymatopora, Ras., 25.
32. ——-, inner surface of broken piece.
33. Cribrillina dentipora, in Bactridium-form, 2,3.
34, 35, 36. Retepora marsupiata, Smitt, 2°.
Pruate XVI.
37, 38. Catenicella solida, sp. nov., 2°.
39. Catenicella cribriformis, sp. nov., 25.
40, 41. flexuosa, sp. nov., 2°.
42, 43. elegans, var. Buskti, 22.
44, 45. marginata, sp. nov., 32.
46. Catenicella ampla, sp. nov., 2°.
47. alata, Thom., 2,5.
48. Retepora rimata, sp. nov., 7°.
49. Catenicella alata, Thom., 2°., dorsal surface.
50. ampla, sp. nov., dorsal surface, 25.
51, 52. Canda fossilis, sp. nov., 2°.
53. Retepora rimata, sp. nov., dorsal surface, 2,°.
54. Mucronella duplicata, sp. nov., #2.
55. Membranipora geminata, sp. nov., **.
56. Schizoporella excubans, sp. nov., 2°.
57. Porina coronata, Rss., 2,5.
58. Catenicella alata, Thom., 25.
Prats XVII.
59. Retepora marsupiata, Smitt, 1,7, basal portion.
60. Lepralia corrugata, sp. nov., 32.
61. Retepora marsupiata, Smitt, 3,2.
62. Cellaria ovicellosa, Stol., 2.
63. Microporella elevata, T. Woods, 32.
64. , seen from the interior, +2.
65. Smittia Tatei, T. Woods, 25.
66. Mucronella mucronata, Smitt, 32.
67. Porina clypeata, sp. nov., 25.
68. Cribrillina terminata, sp. nov., 72.
69. Porella emendata, sp. nov., 3,2.
70. denticulata, Stol., 32.
71. Selenaria marginata, T. Woods, 25.
72. Microporella ferrea, sp. nov., 32.
7d. violacea, var. fissa, seen from the interior, showing the elongate
median pore, 45: a, pore, $5.
74. Membranipora cylindriformis, nev., 22.
75. Cribrillina suggerens, sp. nov., 22.
76. Retepora marsupiata, Smitt, 32. Basal portion.
Gide marsupiata, Smitt, 3,2.
Priate XVIII.
78, 79, Catenicella internodia, sp. nov., 22.
80. Schizoporella excubans, sp. noy., about 4°: a, aperture of ditto, 85.
81. conservata, sp. noy., 2°.
Fig. 82.
2 83.
84,
85.
86.
87.
88.
89.
90.
91.
92.
93.
94,
BRYOZOA FROM 8.W. VICTORIA, AUSTRALIA. 347
Membranipora lusoria, sp. nov., 25.
Microporella see 2ea, sp. nov., 2 .
clavata, Stol.,
Sehizoporella submersd, sp. nov., 35.
Caberea rudis?, Busk, 25.
Lepralia spatulata, sp. nov. fy a
Porina columnata, sp. SOs ars
Cellepora fossa, Hasw., 42,
Microporella elevata, Woods, asa : a, transverse section of growing end.
Mucronella elegans, MacG., 22.
Lepralia cleidostoma, Sm., var. PETE: nov., 3.
Retepora marsupiata, Smitt, 2
Smittia anceps, MacG., 7: a, ae aperture, 5°; 5, aperture seen from
the interior.
Discussion.
The Presivenr stated that the abstract read only gave the main
points of a series of elaborate paleontological descriptions. In reply
to Mr. Charlesworth, he said that Mr. Waters had settled the ques-
tion between Ehrenberg’s name of “‘ Bryozoa” and Thompson’s name
of ** Polyzoa” in favour of the former.
345 R. W. COPPINGER ON SOILCAP-MOTION.
25. On Somcar-Motion. By R. W. Coppinerr, Esq., M.D.
(Read March 23, 1881.)
(Communicated by the President.)
1 wis to call attention briefly to a phenomenon which, so far as I
am aware, exists to an unparalleled degree about the shores of
Western Patagonia, and whose presence there is in a great measure
due to the exceptionally wet nature of the climate. I allude toa
slippage of the soilcap, which is, I believe, continually taking place
over the basement rock wherever the latter presents a moderately
inclined surface. Some of the effects of this soilcap-motion are apt
to be confounded with those due to glacial action; tor the soilcap
takes with it in its progress not only its clothing of trees, ferns,
and mosses, but also a ‘‘ moraine profonde” of rocks, stones, stems
of dead trees, peat and mud, whereby the hills of this region are
being denuded, and the valleys, lakes, and channels, gradually
filled up.
On arriving at the Patagonian archipelago my attention was
directed to this subject on noticing that the lower branches of
trees fringing the sea-shore were in many places withering from
immersion in the salt water, and that in some cases entire trees
had perished prematurely from their roots becoming entirely sub- -—
merged. On looking more closely I observed that the sodden
snags of dead timber, mingled with stones, were often to be seen
at the bottom of the inshore waters, and that the beds of fresh-
water lakes were plentifully strewn with similar fragments of wood,
the remains of forests prematurely destroyed. As the soileap, by
its sliding motion, reaches the water, the soluble portions are
removed ; and just as stones and boulders are often seen deposited
in grotesque situations by a melting iceberg or a receding glacier,
so are the phenomena of ‘perched rocks” to be here observed,
although, in the class of cases to which I refer, due to a totally
different cause. These facts are all the more interesting from their
occurring in a region where the effects of old glacial action are to
be seen in a marked degree. Planings, scorings, striz, and “ roches
moutonnées ” may almost invariably be found wherever the rock is
sufficiently capable of resisting the disintegrating influence of the
weather to retain these impressions. Thus they are nowhere to
be seen on the coarse-grained friable syenite, which is the com-
mon rock-formation of the district; but where this rock is
intersected by dykes of the more durable greenstone, the above-
mentioned signs of former glacial action may be seen well deve-
loped. There are therefore in this region ample opportunities of
comparing and differentiating phenomena which have resulted from
‘‘elacial action” and those which are due to “soilcap-motion ”—a
force now in active operation.
I may here observe that we did not see any glaciers worthy
R. W. COPPINGER ON SOILCAP-MOTION. 349
of the name either on the western islands or abutting on the main-
land shores of Patagonian channels, although they undoubtedly
exist further eastward, and discharge icebergs at the head of some
of the deep fiords. In the main straits of Magellan there are fine
examples of complete and incomplete glaciers, where one may ob-
serve in all its grandeur the wonderful denuding power which these
ponderous masses of ice exercise as they move silently along their
rocky beds.
Sir Wyvyille Thomson (vide ‘ Voyage of the Challenger, the
“ Atlantic,” vol. ii. p. 245) attributes the celebrated “stone rivers ”
of the Falkland Islands to the transporting action of the soilcap,
which, among other causes, derives its motion from expansion and
contraction of the spongy mass, due to varying conditions of moisture
and comparative dryness ; and this hypothesis is to a certain extent
supported by the occurrences which I am now endeavouring to de-
scribe. Here, in Western Patagonia, are evergreen forests, and a
dense undergrowth of brushwood and mosses clothes the hillsides
to a height of about 1000 feet ; and this mass of vegetation, with
its subjacent soil, resting as it frequently does upon a hillside
already planed by ice-action, naturally tends, under the influence
of gravitation, combined with that of expansion and contraction, to
slide gradually downwards until it meets the sea or a lake or valley.
In the first two cases its free edge is then removed by the action of
the water, in a manner somewhat analogous to the wasting of the
submerged snout of a Greenland glacier in the summer time; and
in the last case the valley becomes converted into a deep morass.
It appears to me that the conditions which are said to have
resulted in the production of the ‘stone rivers” of the Falklands
here exist in equal if not greater force. There is the thick spongy
vegetable mass covering the hillsides and acted on by varying con-
ditions of extreme moisture and comparative dryness; there are
the loose blocks of disintegrating syenite to be transported; and
there are the mountain-torrents, lakes, and sea-channels to remove
the soil. Of actual motion of the soileap we have at least strong
presumptive evidence ; but nowhere in the valleys have I found
any thing resembling a “ stone river.”
It might perhaps be thought that a slow and gradual depression
of the land would account for some of the above phenomena ; but
I have seen no reliable sign whatever of subsidence, and have, on the
contrary, the evidence of numerous raised beaches and the work of
stone-boring mollusca at heights above the present sea-level to prove
that elevation of the land has taken place.
The subject is one full of interest ; and feeling confident that it
will repay further investigation, I take this opportunity of bringing
the foregoing observations to your notice.
Discusston.
The Prestpenr said the theory brought forward in this paper
would very well account for some cases of the infilling of valleys,
350 R. W. COPPINGER ON SOILCAP-MOTION.
lakes, and sea-margins, and was especially important as showing how
some phenomena ordinarily attributed to ice could be produced.
Mr. Ussuer asked what the nature of the subsoil was.
Mr. Forpuam asked for information as to the origin of the soil-
cap, and its formation on the high ground from which it was stated
to be slipping.
Mr. Hawxsuaw remarked that engineers, to their cost, were well
acquainted with the unstable condition of the soilcap. Small dis-
turbances often set in motion large masses not only of clays but of
rocks. Good examples of rock-movement might be seen on the
Ripponden branch of the Lancashire aud Yorkshire Railway. The
surface once disturbed, continued to move for long periods. In some
railway-cuttings the slopes had moved for twenty years.
Mr. Sprartine called attention to the slipping of clay in the
Brockley cutting, near new Cross.
Mr. Huptezsron said this paper supplemented Sir Wyville Thomson’s
observations on the “ stone rivers ” of the Falkland Isles, where he
explained the accumulation of quartzite blocks by this kind of slip-
ping. Such observations tended to show how some of the old
brec ciasmight have been formed by other agencies than that of ice.
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 301
26. On the precIsE Mopr of AccuMULATION and Derivation of the
Moet-Tryran Suey Deposits ; on the Discovery of Smmiiar
Hieu-Levet Deposits along the HKasrrrn Storrs of the WELsH
Mountains; and on the Existence of Drirr-zonus, showing
probable Variations wm the Rate of Susmercencr. By D.
Macxintosu, Esq., F.G.S. (Read April 27, 1881.)
ConTENTS.
J. Introductory Remarks on the variable Character of the Lower Boulder-
drift of the Lake District, North Wales, &c.
II. Moel-Tryfan Deposits, &c.
III. Deposits on Halkin Mountain, Flintshire.
IV. Discovery of High-level Deposits of Gravel and Sand between Minera
and Liangollen Vale, Denbighshire.
VY. High-level Gravel and Sand near Llangollen.
VI. Remarks on the High-level Gravel and Sand of Macclesfield Forest.
VII. Arrangement of the Drift-deposits of North Wales into Vertical Zones,
showing probable Variations in the Rate of Submergence.
VIII. Concluding Remarks as to whether the Submergence was caused by
Subsidence of the Land or Rising of the Sea.
I. Inrropuctory REMARKS ON THE VARIABLE UHARACTER OF THE
Lower Bovutprer Drirt or tHE Laxe Disrricr, Norra Wats, &e.
Many years’ observations along the east coast of the Irish Sea, from the
Solway Frith southwards to the estuary of the Dee, have led me to con-
elude (as stated in former papers published in this Journal) that while
the Upper Boulder-clay is a remarkably persistent and homogeneous
formation, and while the line of separation between it and the
cleanly washed, obliquely laminated, and boulderless sand and gravel
(where the two formations are present) is always distinctly marked,
the Lower Boulder formation varies both vertically and horizontally
from compact stony clay to loam, gravel, and sand. This is more
especially the case in the neighbourhood of the mountains and at
comparatively high levels. Around the mountains of the Lake
District (where it is called pinnel) it is often interstratified with or
replaced by well-laminated and often contorted sand and gravel, as
at Ulverston Railway station, between Ulverston and Arrad Foot,
&ec. Inthe neighbourhood of Bangor, though a stiff Boulder-clay
may here and there be seen lying under stratified sand and gravel,
the two kinds of drift may quite as often be found in horizontal
succession ; and they both agree in containing boulders (see VII.
1 and 2).
II. Mort-Tryran Deposrts, &e.
1. Bruef History of Discovery.—In 1871, and again in 1880 (last
year), I had opportunities of tracing the drift-deposits of Caernar-
vonshire from the neighbourhood of Bangor to the top of Moel
Tryfan, and of observing a number of facts connected with the Moel-
352 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
Tryfan deposits which would appear to have escaped the notice of
previous observers. But before proceeding to the main subject, it
may be desirable to give a brief account of the discoveries made since
the first published account of the deposits.
Trimmer, in the ‘ Proceedings’ of the Geological Society for 1831,
has a short notice of the Moel-Tryfan drifts, in which he found Bucei-
num, Venus, Natica, and Turbo (if correctly identified) beneath 20 ft.
of sand and gravel. In vol. i. of the ‘ Journ. of the Geological Soc.
of Dublin’ (1838), he wonders if the granite as well as the flints he
found on Moel Tryfan came from Ireland. [He heard of quarrymen
finding sea-shells on Moel Faban, near Bethesda, where Darwin
afterwards could find no trace of drift likely to contain shells.| In
his work on Geology, published in 1841, Trimmer gives a general
section of the drift from Menai Strait over Moel Tryfan to Mynydd
Mawr. He could find granite erratics only at eight points between
Menai Strait and Snowdon.
Buckland, in 1841, found rounded chalk-flints and white granite
in the Moel-Tryfan deposits. His paper was read before the Geo-
logical Society, and an abstract of it appeared in the ‘ Athenzeum,’ in
1842.
Darwin, in 1842, in the ‘ London, Edinburgh, and Dublin Phi-
losophical Magazine and Journal of Science,’ gives a very sug-
gestive description of the Moel-Tryfan deposits. He found boulders,
chiefly from the neighbouring mountains, but likewise rounded flints
and white granite. Under the drift he saw that the surface of the
slate, to a depth of several feet, had been shattered and contorted in a
very peculiar manner. He did not find shells; but near the summit
of the hill, on the east side, he saw a thickness of at least 20 ft. of
irregularly stratified gravel with boulders and layers of sand and
fine clay. He attributed the shattering and contorting of the slates
to icebergs grating over the surface, and lifted up and down by the
tides. The shattered and rounded slate rocks were similar to what
he had seen in Tierra del, Fuego. He believed that the Chalk tints
had been brought by floating coast-ice.
Darbishire gave an account of the Moel-Tryfan deposits in the
‘ Proc. of the Manchester Lit. and Phil. Soc.’ for 1851-52, and in
the ‘Geol. Magazine,’ vol. ii. He believed that a layer of yellowish-
brown sandy clay 1 ft. 9 in. thick had preserved the shells in the
underlying sand and gravel. He collected a great number of shells,
a list of which may be found in Mr. Shone’s paper in the ‘ Quart.
Journ. Geol. Soc.’ for May 1878, and in Dr. Gwyn Jeffreys’s paper
in the same Journal for Aug. 1880.
Lyell and Symonds, in 1863, visited Moel Tryfan, and found a
mass of incoherent.stratified sand and gravel, 35 ft. thick, with
fragments of shells, and a few whole specimens. In the lower beds
they saw several large boulders of far-transported rocks glacially
polished and scratched on more sides than one.
Ramsay and Etheridge, in 1876, examined the Moel-Tryfan de-
posits, and found that the boulders were chiefly local, and that the
sand and gravel were obliquely laminated, similar to what may be
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTs, 353
seen on a sea-beach. Ramsay gives a comprehensive account of the
deposits in the last edition of his ‘ Physical Geography and Geology
of Great Britain.’ He specifies the indirectly local erratics sw Bich
came under his notice, and regards the mountain from what may be
called the Snowdon stand-point. Though he had previously observed
the drift-sections (in 1852), it would appear that the curved slaty
lamine which I have been led to regard as the most interesting of
all the Moel-Tryfan phenomena, were not during his visits, or indeed
during the visits of any other geologist excepting Darwin, sufficiently
striking to arrest attention, In this paper the mountain will be
principally regarded from the N.W. and N. stand- -points.
2. Deposition during Submergence.—lt seems to be generally
admitted that deposition is in excess during submergence, and denu-
dation during emergence ; and when we consider the thickness of and
area covered by the Moel-Tryfan deposits, in connexion with the
fact that they lie on a sloping surface, and reach up to within a short
distance of the rocky crest of the hill, the idea of accumulation during
the submergence or sinking of the land appears the most probable,
while it is the most consistent with certain facts to be mentioned i in
the sequel.
3. Identification of the Local and Erratic Stones—The most pre-
valent pebble, rock-fragment, or boulder in these deposits is a light-
coloured felstone, which may have come from the Cambrian conglo-
merate of the upper part of the hill, or from adjacent hills. The
fragments of talcose or chloritic schists must have come from rocks
like those which are now found in the tunnel (near the top of the
hill), or from similar rocks in the hills around Moel Tryfan. The
basaltic-looking diorite or greenstone may have come from bands in
the hill or adjacent hills. Many small quartz pebbles in the drift
may have come from the Cambrian conglomerate already mentioned*.
The numerous fragments of slate may be very nearly i situ, or may
likewise have come from neighbouring hills. There are many
Eskdale granite pebbles, and a smaller number of granite pebbles
from the south of Scotland (chiefly Criffel). Chalk flints are rather
numerous (during my last visit they predominated in a particular
part of the excavation), and reach a height of about 1350 feet.
Eskdale granite on Moel Tryfan is found up to at least 1350 feet
above the sea, or 64 feet above the highest range of the rock zn situ.
Chalk-flints i situ, in Ireland, as Professor Hull has informed me,
do not rise higher than about 1000 feet above the sea; so that on
Moel Tryfan their height is 350 feet higher (see VIII.). On Moel
Tryfan I found a pebble of red granite of unknown derivation, but
exactly of the same kind as one I saw on the beach of West Cum-
berland, and one on the Blackpool beach.
4. Arrangement of the Gravel and Sand.—Most writers on the
Moel-Tryfan deposits have noticed the extent to which the sand and
fine gravel are obliquely laminated, and the resemblance they bear
to what may be seen on a sea-beach. The sand is often as fine as
* JT have to thank Dr. Hicks for assisting me in tracing the derivation of the
local and indirectly local stones.
304 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
blown sand, and, when I last saw it, was in course of being blown
by the wind, from the brink of the quarry-excavation, over the grassy
flat above. On the right-hand side of the tunnel, where there is no
clay above the sand, the latter presents a peculiarly involved
appearance.
On the left-hand side of the tunnel (1880) the sand inter-
laminated with gravel had evidently been contorted to a great extent.
The shell-fragments principally occurred in layers of fine gravel, in
one place chiefly made up of angular flint chips. There the average
thickness of the sand and gravel was about 10 feet, the clay above
being about the same thickness. When Darbishire saw these drifts
about thirty years ago the clay was only about 1 ft. 9 in. thick. In
different quarry-excavations at different levels up the hill-side, sections
more or less differing in their character have been revealed. In
1880 the brink of the drift-cliff was only about 30 feet below the base
of the abruptly rising rocky crest of the hill; and it is more than
probable that the crest once rose as an isolated mass of rock above
the surface of the glacial sea. The shelly sand and gravel (so far
as aneroids can be trusted) extend up to quite 1350 feet above
the present sea-level; and they have been found as low down as
1170 feet.
5. Position of Boulders.—One may go for miles along a railway-
cutting without seeing a single boulder in situ ; but where a large
clay- or gravel-pit has been excavated by the side of the railway,
many boulders may be seen on the floor of the pit, the explanation
being that boulders exposed in a railway-bank very soon tumble
down and are covered up, blasted, or removed. It is therefore wrong
to conclude that because there may be many boulders on the floor
of a quarry in drift-covered rock, they were (as boulders) originally
situated at the base or towards the base of the drift-deposits. Itis
probable that many of the boulders of the Moel-Tryfan deposits
which now lie on the quarry floor, were once dispersed at various
levels in the overlying drift ; and in 1871 I saw a boulder at least
3 feet long high up in the sand. This accords with the fact that at
lower levels, including Anglesey, very large boulders may sometimes
be found imbedded in sand or fine gravel containing shell-frag-
ments, as well as in clay.
6. Bent and shattered Hdges of Slaty Lamine. ata 1871 I noticed
that the edges of the vertical slates were bent in the direction of
Mynydd Mawr, or from about N.W. to S.E. Darwin, as already
stated, observed somewhat similar phenomena in 1842, which he
attributed to the impact of floating-ice. In 1880 I happened to see
what may be called a magnificent display not only of the bending
but likewise of the shattering of the edges of the slaty lamin, and
of the extreme contortion of the laminz of sand by which the slates
were covered (fig. 1). From the section (which from the quarry upper
floor to the top of the clay is at least 20 feet thick) it is perfectly clear
that the sand and overlying clay must have been deposited before
the derangement of the clay, sand, and slaty laminee took place.
The only ‘explanation which appears sufficient to account for this
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. B13)3)
derangement is the violent stranding of an iceberg or mass of floating
ice from the N.W. on the previously accumulated clay, which it
pressed forwards and downwards until it reached the sand, which it
ploughed up and inverted, and then bent and shattered the edges of
the slaty laminz, so as to be able to roll up parcels of clay and
slate-chips in the sand. The line marking the commencement of
the slaty curvature is nearly horizontal ; but the upper termination
inclines slightly in the direction of the movement of the floating ice
(at first probably raised a little above the level of flotation by the
impact, and afterwards shghtly lowered so as to regain its normal
level). This section bears no real resemblance to some which are
found in districts where traces of ice-action are absent, and which
are believed by some geologists to have been caused by ordinary
atmospheric action. On Moel Tryfan the finely laminated sand shows
no trace of having ever been disturbed by the percolation of rain-
water or by frost, while the preservation of the numerous shell-
fragments in continuous though contorted layers of sand and fine
gravel has evidently (as Darbishire long ago pointed out) been
owing to the clay preventing the downward passage of rain-water.
As Moel Tryfan is in the midst of a glaciated district, and as ice
-eapable of bending the slates and contorting the sand must have
brought the erratic stones, including chalk-flints from Ireland, why
have recourse to any other supposition to account for the phe-
nomena ?
Fig. 1.—Laminated Sand and Bent Slates on Moel Tryfan.
8.E. NW.
9
1S]
Sat
Ts
lates ; B B, Sand, with parcels of slate-chips and Boulder-elay ;
renin
AA,
op)
7. Direction of Floating Ice in Ireland.—According to the Rev.
M. H. Close the principal direction of floating ice in Ireland during
the glacial submergence was from about N.W. to S.E. ; so that the
local floating ice would only have to persevere in this direction,
after leaving Ireland, in order to reach Moel Tryfan.
8. Were all the Moel-Tryfan Shells brought by Floating Ice ?—
This idea would appear to be untenable for the following reasons :—
(1) The shells must at first have been somewhere én situ, and why
not on Moel Tryfan? (2) The Mollusca may have lived where the
erratic stones were imported as well as where they were exported.
396 D. MACKINTOSH ON HIGH-LEVEL MABINE DRIFTS.
(3) Shells have not been found in Eskdale on the old sea-coasts from
which the granite erratics on Moel Tryfan were transported when
the land was deeply submerged (see 11).
9. Cause of the Absence of similar Deposits on the Lower Slopes of
the Hill.—It has often been remarked that beach-like deposits with
shells have not been found on Moel Tryfan excepting towards the
summit of the hill. It is perhaps too early to speak positively on
this point, as there is a bare possibility of patches of such deposits
being yet discovered. But the cutting for the railway above Bryn-
gwyn, which extends from near the base to near the summit of the
hill, shows no trace of laminated sand and rounded fine gravel, but,
on the contrary, is everywhere a Boulder-clay, or clayey loam, with
stones, chiefly angular or subangular. The drift on the north side of
the hill, so far as revealed by cart-roads, is somewhat similar to that
above Bryn-gwyn, excepting towards the summit, where there are
patches of gravel and sand interstratified with clay and loam. The
cause of the difference in the deposits near the summit and lower
down cannot (at least principally) be a difference in the sources of
supply of the lower and higher drifts, because the materials for the
elaboration of fine sand and gravel exist on the hill-slopes at low as
well as at high levels. The most probable explanation seems to be
that the submergence of the lower slopes of Moel Tryfan went on too
rapidly to allow sufficient time for the accumulation of well-rounded
beach shingle and sand (see sequel).
10. Moel-Tryfan Shells and Erratics not pushed up hill by Land-
1cé.—It has been asserted (though this is not the general opinion)
that all the shells, along with the erratic stones, were pushed out
of the bed of the Irish Sea as far south as Moel Tryfan, and then
up the hill-slopes nearly to the summit by land-ice. But an inti-
mate acquaintance with the character of the Moel-Tryfan deposits
precludes this idea; for, if it were a true explanation, the shells and
erratic stones would have diminished in number the higher up they
were pushed. but, on the contrary, the shells and erratics in the
drifts near the sea are fewer in number than on Moel Tryfan.
This theory would likewise require to invest the land-ice with the
power of rounding the pebbles derived from the upper part of the
hill, and laminating the sand and fine gravel; for it ought to be
remembered that though the sand and gravel are, in places, much
contorted on Moel Tryfan, the contortion was evidently, in many
instances, produced after their accumulation.
11. Shells found by the Author.—As my main object was not to
look for shells, only the following nine species were named for me
by Dr. Gwyn Jeffreys out of a number of fragments I collected :—
Cardium echinatum. Tellina balthica.
edule. Mactra solida, var. elliptica.
Cyprina islandica. Saxicava rugosa.
Astarte suleata. Purpura lapillus.
borealis.
It is quite consistent with the remark made in section 8, that
some of the Moel-Tryfan shells may have been brought along with
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 315i
erratic stones from a distance by floating ice, provided we admit that
Moel Tryfan may have returned the compliment; and a number of
shell fragments which I found along with small flint chips certainly
looked as if both had been brought and deposited at the same time,
though their final juxtaposition in the lamina to which (in that part
of the section) they were limited must evidently have been the
result of rearrangement on the spot.
12. High-level Gravel and Sand im other parts of Caernarvon-
shire.—Near the summit-level of the pass of Llanberis, some years
ago, | saw a striking section of obliquely laminated sand and fine
gravel, probably about 1000 feet above the sea-level. The extent to
which the stones were rounded, the arrangement of the lamin, and
the position of the deposit (being away from any channel which
could have conducted a freshwater stream), all pointed to its being
of marine origin, though I did not see any shells. Above Bethesda,
near a farm-house marked Gwaun-y-gwiail on the Ordnance map
(probably about 1000 feet above the sea), a gravel-pit shows lami-
nated and contorted gravel and sand, in which (for reasons which
need not be stated) I had not time to look for shells; but Trimmer
told Ramsay that he had found shells in that neighbourhood up to
from 1000 to 1200 feet above the sea. It does not seem to be
well known that Ramsay found shells in Boulder-clay on Fridd
Bryn-mawr (west of Llanberis) at a height of about 1000 feet above
the sea.
13. High-level Gravel and Sand wm Ireland.—It may be neces-
sary to complete this account of high-level marine drifts in the
western part of Wales by adding a brief statement of what Close
found on the Three-rock Mountain near Dublin (see Geol. Mag. vol. 1.
Decade ii. 1874). He collected shells from gravel-pits at 850 feet,
1000, 1100, and a little higher than 1200 feet above the sea.
The Three-Rock Mountain consists of granite; but the stones com-
posing the gravel were very nearly all limestone, which must have
been brought by floating ice from the N.W. ‘They were nearly all
subangular; but the deposits partly consisted of clean stratified
gravel and sand [showing the action of the sea on the spot?]. He
believed that the shells were brought along with the stones by
floating ice, because both were scratched. He found more or less
clay above the shelly deposits, and was led to believe that the
mountain must have been submerged up to 1760 feet. The Three-
rook Mountain is related to Moel Tryfan by the altitude of its shelly
drifts, and by the direction of the floating ice which brought its
erratic stones.
Ill. Depostrs on Hatxin Mountain, FLINTSHIRE.
Several years ago I read an account of these deposits before the
Chester Natural-Science Society. Since then they have been mapped
by the Geological Surveyors. The mountain, including its westerly
continuation as far as the Vale of Clwyd, is a plateau surrounded on
all sides by lower ground, so as to render it certain that the mounds
Q. J.G.8. No. 147. 23
358 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
of gravel and sand on its summit could never have been accumulated
by the action of fresh water flowing onto it from a higher level. The
mounds range from about 750 to about 900 feet above the sea. The
rounded stones they contain are chiefly local limestone and grit of
Carboniferous age; but Eskdale granite and Lake-District felstone
may be found in some places, and chalk fiints may occasionally be
seen. The most striking mounds in which excavations have exposed
sections are one situated near Brynford (not far from Holywell)
and another towards the 8.E. end of the mountain. The latter is
named Moel-y-Crio on the Ordnance map, and rises from the
summit of a ridge about 950 feet above the sea, with ground falling
all around it, except on one side, where for some distance it is
nearly horizontal, and then falls to a lower level. It would appear
to have been accumulated not so much by wave-action as by the
piling agency of sea-currents while meeting or parting.
Fig. 2.—Perched Gravel-mound on Halkin Mountain.
The Halkin-Mountain deposits of gravel and sand occur at a
lower level than the other high-level marine drifts described in this
paper; and they are not very distinctly separated (excepting, in
most places, along the east side) from the low-level gravel and sand,
which extends upwards from the sea-coast, and inland along the pass
between Mold and Bodfari, which is traversed by the Chester and
Denbigh Railway. Exceedingly few shell-fragments have been
found in the gravel and sand of Halkin Mountain ; but its compara-
tively flat summit, in places surrounded by ridges, must have been
very favourable to the accumulation of rock -fragments derived from
the inner slopes of the ridges; while it is easy to understand that
these fragments, instead of being washed down the mountain-sides
into deep water, would remain for a considerable time at the mercy
of sea-waves, so as to become more or less rounded and smoothed by
attrition. It ought likewise to be remembered that the mountain,
while an island, must have been exposed all round its coasts to
winds, which, by increasing the power of breakers, may have expe-
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 359
dited the process of rounding stones; so that in the case of the
summit of this mountain (which is situated at a lower level than
that of the gravel and sand on Moel Tryfan, Frondeg, Macclesfield
Forest, &c.) it is not necessary to suppose that the land subsided
more slowly than at the levels immediately below and above, so as
to afford more time for elaborating rounded gravel and sand. As
already hinted, the scarcity of shell-fragments accords with the
idea that the rate of submergence was not sufficiently slow to allow
much time for the growth and accumulation of Mollusca. It ought
likewise to be stated that on many parts of the mountain the stones
in the grayvel-beds are not much rounded.
LY. Discovery oF HigH-LEveL Depostts oF GRAVEL AND SAND
BETWEEN MINERA AND LLANGOLLEN VALE, DENBIGHSHIRE.
For a long time, while travelling by railway between Wrexham
and Ruabon, I fancied, from the suriace-configuration of the eastern
or outer slope of the range of mountains between Minera and Llan-
gollen vale, that marine gravel might there be found at about the
same height as on Moel Tryfan; but, being then bent on finding
sea-shells at higher levels than the Moel-Tryfan deposits, I did not
explore the district until near the close of last year (1880). From
the railway, for some distance westward, the ground is flat or gently
undulating, with an average elevation of between 300 and 500 feet.
In many places sand may be found under a deposit which is hori-
zontally continuons with the upper Boulder-clay of Cheshire; and
here and there the sand, graduating into gravel, rises in the form
of mounds or knolls. From the commencement of the gradual rise
of the ground in a westerly direction up to about 1000 feet the pre-
vailing drift is a clay or loam, with angular stones and large Carbo-
niferous-grit boulders from the mountain-range above mentioned.
At about 1000 feet the ground rather suddenly rises, and the stones
(as may be seen in ploughed fields &c.) become more or less rounded.
A little west of Braich, in the district called Frondeg (see 1-inch
Ordnance map), the ground abruptly swells into a series of ridges
and hillocks, which consist of well-rounded gravel and sand.
1. Surface-configuration and Character of the Deposits—In the
Frondeg district the gravel and sand knolls, with intervening or ed-
jacent deposits of a similar character, extend for about a mile and
a half from north to south, and about one third of a mile in breadth
from east to west; but as similar accumulations are repeated at inter-
vals as far south as Mountain Lodge, the whole length of the deposits
may be about three miles—that is, supposing they extend no further
south. On walking from Braich to the summit of the mountain-range
in a westerly direction, after passing the gravel mounds, the surface
becomes very flat and covered with peat. ‘The breadth of the flat
(which in some places extends, with a very gentle ascent, as far as
the summit of the ridge, in other places not quite so far) is about
half a mile. So far as can be seen in brook-channeils, the peat
overlies a deposit of clay with angular stones and large angular
2B 2
360 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
boulders. The summit of the ridge varies from about 1450 feet to
about 1500 feet. The well-rounded gravel-and-sand commences
about 1100 feet (west of Braich), and extends in a westerly direction
up to about 1350 feet. The hillocks (west of Braich), in one of
which I found numerous shell-fragments in a grayel-pit, range in
height from about 1100 feet to about 1250 feet. Above Mountain
Lodge (8. of Frondeg) there is a gravel-pit in a knoll about 1200
feet above the sea, and one further west (in which I found shell-
fragments) about 1230 feet. But the plateau, near the south edge of
which these pits are situated, consists of rounded gravel-and-sand,
which, in a westerly direction, rises to at least 1350 feet above the
level of the sea*. In the gravel-pits and in the neighbourhood
where sections are exposed in brook-channels, the stones, especially
in the Frondeg district, are very much rounded, more so, in fact,
than on the shores of the Irish Sea, where many of the stones (being
derived from drift-deposits) have undergone a double process of
rounding. This is the case especially with the Hskdale-granite
pebbles, which, in the Frondeg gravel-pit, are almost as numerous
as the local pebbles of Carboniferous grit or sandstone. In addition
to these, there are chalk-flints, pebbles of Lake-district felstone
and felspathic breccia, and local pebbles or fragments of Carboni-
ferous limestone, with much decomposing coal and many coal-measure-
fossils, which can be best accounted for by supposing them to
have been locally worked up from strata now concealed under the
drift-deposits. In the Mountain-Lodge gravel-pits there are many
Carboniferous-limestone fossils, and much granite.
2. Shell-fragments. --In the Frondeg gravel-pit shell-fragments
are very numerous, but I could find no whole specimens. This can
readily be explained by supposing that the excessive attrition to
which the extra-rounded pebbles were subjected must have extended
to the shells which were thrown up on the sea-beach. Among the
fragments I collected from the Frondeg gravel-pit, and partly from
one of the Mountain-Lodge gravel-pits, Dr. Gwyn Jeffreys has
identified the following species :—
Cardium echinatum, Linné. Tellina balthica, L.
C. edule, Z. Mactvra solida, L.
Cyprina islandica, L, Mya truncata, L.
Astarte borealis, Chemnitz. Fusus antiquus, Z.
3. Position of Boulders—So far as can be seen in the grayel-
pits and brook-sections, the large angular boulders are chiefly to be
found in the clay, which extends under peat, from the west border
of the gravel-hillock zone up to near or (in some places) quite to the
summit of the mountain-range. They are likewise found, some-
times thickly strewn, on the surface of the clay, and to a less
extent on the surface of large mounds, which partly, at least, con-
sist of rounded gravel. They may also be seen scattered over the
lower country as far east at least as the railway. In the Frondeg
* T have to thank the Director of the Ordnance Survey, Southampton, for
some of the above heights.
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS, 361
district, where they consist of Carboniferous grit or sandstone
(and partly of quartzose conglomerate), many of them must have
been floated in an easterly direction from near the summit of the
mountain-range after the submergence had reached that altitude ;
for how otherwise can their position on the surface of the drift-
deposits be explained ?
4. Junetion of the Arenig-felstone and Eskdale-granite Dispersions.
—West of Frondeg, on the summit-level of the mountain-range, about
1500 feet above the sea, and extending a short distance eastwards,
the stones, with the exception of those of local derivation, consist of
Arenig felstone ; and large boulders of the same felstone are found
on or near to the summit of the range further south, as well as
strewn over the whole district between there and the Great Arenig
mountain. I was surprised to find so great a number of Arenig
pebbles on the ridge west of Frondeg, and equally surprised to dis-
cover that they abruptly terminated in an easterly direction not far
from the water-parting, where their place (with very little dove-
tailing) was taken by Eskdale granite, reaching up to about
1400 feet. I arrived at the conclusion that there the northern-drift
current which floated the Eskdale erratics was sufficiently powerful
to turn aside the current by which the Arenig erratics were floated
from the west. I cannot believe that the latter could have been
brought by land-ice, because 1b appears improbable, if not impos-
sible, that land-ice proceeding from the Arenig mountain could
have attained a surface-level of 1500 feet (above the present sea)
by the time it reached the ridge west of Frondeg; and it may like-
wise be remarked that as Arenig erratics have been found, not far
from this ridge, on Cyrn-y-brain up to a height of 1830 feet, the
supposed land-ice which brought them must have reached as high as
that level, while further S8.W., on Moel Gamelin, it must have
reached to about 1900 feet*. This is about the limit reached by
the glacial submergence in the N.W. part of Wales, where (as well
as in the Frondeg district) the upward termination of the zone of
rounded gravel-and-sand may be explained by an increased rapidity
in the rate of submergence having deprived the sea of the time
required to round stones by a process of combined rolling and
attrition +.
5. Frondeg Erratic Stones and Shells not transported by Land-
* See my paper on the Boulders of North Wales in Quart. Journ. Geol. Soe.
vol. xxx. (1874), p. 711.
t Mr. 8. V. Wood, F.G.S, has written to me to the effect that he regards
the discoveries I made in the Frondeg district as corroborating the conclusion
at which he arrived after reading my paper on boulders (Quart. Journ. Geol.
Soc. vol. xxxv. (1879), p. 425), namely that land-ice extended from the Arenig
mountain to the top of the ridge west of Frondeg, on which it left the Arenig
erratics ; while floating ice from the Lake Districs brought the Eskdale erratics
to the edge of the land-ice which prevented them from reaching further west, at
the time when the submergence culminated at about 1400 feet. Mr. Wood
likewise believes that the land-ice of the central part of North Wales spread
out towards the N.K. and north, so as to prevent the erratics brought by floating
ice from the north from getting into the interior of the country.
362 D, MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
wce.—The idea of the granite pebbles of the Frondeg dis-
trict having been brought by land-ice is opposed by the fact
that few HEskdale-granite pebbles (so far as I have noticed) are
to be found between Frondeg and the estuary of the Dee (the
direction in which the ice would most probably move) excepting
near the Dee estuary. There is likewise an equal absence of shell-
fragments in the drift-deposits where the latter are present; but
it is a remarkable fact that a great part of the area intervening
between Frondeg and the Dee estuary is free from drift. Sup-
posing the erratics and shells to have been pushed forward under
the ice, they ought to be represented over the whole, or at least the
greater part, of the intervening area, while no one would suppose
that the numerous extra-rounded pebbles of Frondeg could have
come in the form of a supraglacial moraine.
6. Probable Decrease in the Rate of Submergence.—It has already
been remarked that from about 500 feet to about 1000 feet on the
east side and flanks of the mountain-range under consideration the
stones in the drift are generally angular or subangular, while
above 1000 feet they are generally rounded, and in many places
extra-rounded. Itis likewise true that of the standard Frondeg
erratics, namely Eskdale-granite, not one in fifty can be found in the
comparatively low-level drifts between the mountain-range and the
railway, while in the Frondeg district, above 1000 feet, Eskdale-
granite pebbles are very numerous. We have no reason for sup-
posing that the sea in this latitude was sufficiently warm to melt
the floating ice, so as to cause the precipitation of many erratic
stones. On the contrary, the great number of granite pebbles
which have found their way as far south as Shrewsbury (where they
are rather numerous in the lower Boulder-gravel, though not in the
upper clay), and the much greater number (within a limited
breadth of area) which reached as far south as Burton (S.W. of
Broseley)* would seem to indicate that where many of these
pebbles are found crowded in a small compass (as in the Frondeg
district) they were left by the stranding and consequent breaking-
up of floating ice. At this period the district was probably in the
condition of a littoral zone, which may have lasted for a time
sufficient to enable the waves to round the stones and to allow
the Mollusca to multiply in the littoral and sublittoral zones, and
thereby furnish many shells destined to be reduced to fragments by
the rolling and grinding of stones on a much-exposed sea-coast.
But a protracted sojourn of sea-waves in what is now the Frondeg
district is hkewise indicated by the time required for the accumula-
lation of the immense number of erratic stones. That these
stones were rounded approximately in setw is evident from the fact
that at the high levels in the Eskdale district, from which the
stones must have been launched, the stones are all more or less
angular.
* See Quart. Journ. Geol. Soe. vol. xxxvy. (1879). p.425. The Frondeg erratics
are not mentioned in this paper, as I had not discovered them when the paper
was written.
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 363
V.—HieH-LEVEL GRAVEL AND SAND NEAR LLANGOLLEN.
Around Llangollen and elsewhere in North Wales a kind of
loamy clay, or clayey wash, often forms the surface of the ground,
and conceals what lies underneath. It may have been partly
deposited as the land sank into deeper water, and partly during the
rising of the land. The existence of an unknown extent of gravel
and sand under this clay at a high level might never have been dis-:
covered but for the excavation of a pit a short distance east
of Rhos Pengwern farm, in a field nearly 1200 feet above the
sea-level. Under about 3 feet of clay, with perfectly angular
stones, there is an unknown thickness of fine and coarse gravel and
sand arranged in lamine more or less arch-shaped. The stones are
considerably rounded and smoothed, though the sand does not
appear to have been very cleanly washed. ‘There can, however, be
no doubt about its being a sea-coast or shallow-sea deposit (though
I could not find any shell-fragments), as its situation precludes the
idea of its having been accumulated by any freshwater stream.
More extensive excavations are required to show both its horizontal
and vertical extent. At lower levels down to about 500 feet or
400 feet above the sea the drift contains scarcely any rounded
stones, while it is particularly worthy of remark that in a pit at
the east end of Grouse-box Hill (not far from Pengwern pit) about
1300 feet above the sea, the gravel is perfectly angular, and con-
tinues so up to the summit of the hill, 1715 feet above the sea.
VI.—Remarks oN THE HigH-LEVEL GRAVEL AND SAND OF
MaccLEsFIELD Forsst.
The identity in level of the Frondeg and Macclesfield-Forest
deposits renders it appropriate that some notice should be taken of
the latter. They were discovered by Professor Prestwich in 1862,
near the Setter Dog Inn, at an altitude between 1100 and
1200 feet above the sea. He found more or less clay both below
and above the shelly gravel and sand; but I should be inclined to
regard the clay above as on a horizon distinct from that of the
upper Boulder-clay of the plain of Cheshire, and more or less allied
to the patches of clay or loam which overlie the high-level gravel
and sand of North Wales. I found the shelly gravel near the
Setter Dog Inn graduating eastward and upward, in the direction of
Shining Tor, into angular gravel at a height of more than 1350 feet
above the sea. At a greater height, in an easterly direction, all the
gravel is angular; but S.E. of the Setter Dog, in Chapel Lane,
rounded erratics may be found up to about 1400 feet. From these
facts it would appear that the two gravel districts, the one on the
west (Frondeg), and the other on the east (Macclesfield Forest), cor-
respond almost exactly in level—Near Clulow Cross, some distance
south of Macclesfield Forest, Mr. Sainter (of Macclesfield) has dis-
covered gravel and sand with sea-shells about 1130 feet above the
sea (see his interesting work entitled ‘Rambles round Macclesfield’),
364 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
So far as I can recollect, the western slopes of the Penine hills
between the above-mentioned levels and the plain of Cheshire are
comparatively, if not entirely, free from rounded gravel; but I
hope to have an early opportunity of speaking with certainty on
this subject.
VII.—ARRANGEMENT OF THE Drirr-pEposits orf Norra Watzs
INTO VERTICAL ZONES, SHOWING PROBABLE VARIATIONS IN THE
Rate oF SUBMERGENCE.
The existence of the above rounded gravel- and sand-deposits,
with shells, at about the same level in different parts of North
Wales, and likewise in England and Ireland, could scarcely have
been the result of accident. At a somewhat lower level than these
deposits the drifts are angular, with a few exceptions, which may
have arisen from local conditions having been unusually favourable
to the rounding of stones by rolling and attrition. Above the level
of the shelly deposits rounded gravel and sand with shells would
appear to be everywhere absent. If the time required for rounding
stones be viewed in connexion with that necessary for the migration
and multiplication of Mollusca (as already remarked), it will not
appear too fanciful to suppose that the rate of submergence was
slower (probably much slower) in what may be called the rounded
gravel and shelly zone than in the zones above and below, especially
as it 18 a priort improbable that the submergence (up to at least
1350 feet above the present sea-level) progressed at a uniform rate.
Many believe that the submergence terminated at the upper lmit
of this zone ; but, as long ago advocated by Professor Ramsay, and
recently repeated in his ‘ Physical Geography and Geology of Great
Britain,’ a clay similar to that in which he found shells west of
Llanberis may be seen rising to a height of from 1500 feet to
1800 feet about the Turbary, and east of the river Ogwen. I noticed
that the drift between the Turbary and the final ascent to
Marchllyn Mawr (about 1700 feet) consisted either of clay or small
chips and fragments arranged in a manner which could not possibly
be explained by the action of fresh water; and in a continuation of
this drift at a lower level the late Mr. Griffith Ellis, of Llanberis,
told me he had discovered sea-shells. In the basins of the Llafar
and Caseg (S.E. of Bethesda) the general surface-configuration of
the ground up to about 1900 feet can be more easily explained by
the former action of the sea than by freshwater agency; and this
accords with the height reached by the Arenig boulder-dispersion
in the nighbourhood of Llangollen (1897 feet on Moel Gamelin)
and on the neighbouring hill-sides. In the present state of dis-
covery it may therefore be said that the glacial submergence
certainly reached an altitude of about 1350 feet (the extreme
height at which sea-shells have been found), and very probably
culminated at about 1900 feet. Below the middle (or Moel-
Tryfan, Frondeg, and Macclesfield-Forest) zone of rounded and
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 365
shelly gravel and sand, as already stated, there would appear to be a
zone consisting of loam, with angular or subangular stones and no
shells; but this zone is not uniformly continuous, as on Halkin
Mountain (Sec. III.), and possibly in other places; it is varied by
accumulations of more or less rounded gravel and sand. Below the
third zone (order descending), and extending down to the existing
sea-level, there is a zone of horizontally alternating clay, and
angular and rounded gravel and sand, with boulders and shells*.
Causes of the horizontal Discontinuity of the Middle Zone of
rounded Gravel and Sand.—The question may naturally be asked,
How is it that the rounded and shelly drift of Moel Tryfan,
Frondeg, and Macclesfield Forest are horizontally separated by
areas in which the drift is angular? We may, I think, be enabled
to arrive at some explanation of this fact by supposing that rounded
drift on this horizon may exist in many places under a covering of
Boulder-clay, which may have been wholly or partly left during
the rising of the land; but there are other considerations which
might account for the local absence of rounded drift, one of them
being that the sea, by merely lingering for a time near the same
level, might not be able to accumulate rounded drift without being
assisted by other favourable circumstances or conditions (positive
or negative) such as the following :—(1) a sea-coast exposed to
wave-producing winds; (2) the previous or contemporaneous
accumulation of heaps of angular débris by melting or stranding
icebergs or coast-ice, frost, rain, gravitation, &c.; (3) the absence
of steep slopes which would so facilitate the washing-down of pre-
existing angular débris below the reach of wave-action as to pre-
vent the accumulation of rounded stones} ; (4) the absence on sea-
beaches of clay, which would be unfavourable to the rolling of
stones ; (5) the prevalence of stones susceptible of being easily
rounded; (6) the existence of rapid currents capable of rolling
stones below the limit of wave-action ; (7) the preservation of
relative levels of the differently characterized zones during the
emergence of the land; (8) the non-alteration of the character of
the zones by deposits left during emergence; (9) the non-removal
of preexisting rounded gravel and sand from valleys and slopes by
glaciers during or after emergence. The last consideration is very
important ; for, according to Professor Ramsay (to the great accu-
racy of whose observations in North Wales I can bear humble
testimony), the marine drift of the northern valleys was ploughed
out by the second glaciation of the country.
* Tt might unnecessarily complicate the main subject of this paper were I to
_ refer particularly to a zone of fine rounded gravel and sand, with no boulders,
at a low level in the plain of Cheshire and part of Lancashire (which I believe
was deposited during the last stage in the rising of the land), or to the upper
Boulder—clay at comparatively low levels, which I believe was the result of
a re-submergence of the land. I lately found proofs of a land-surface between
the upper Boulder-clay and underlying boulderless sand in excavations under
Crewe railway-station, an account of which will soon be published.
+ On the very steep slope of Mynydd Mawr, which is nearly opposite to the
marine drift on Moel Tryfan, the stones are all angular.
366 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
VIII.—Concivpine REMARKS AS TO WHETHER THE SUBMERGENCE
WAS CAUSED BY THE SUBSIDENCE OF THE LAND OR RISING OF
THE SEA.
In favour of the extension to the district under notice of Dr.
Croll’s theory of a rise of the sea-level by the melting of circum-
polar ice, and consequent displacement of the earth’s centre of
gravity, and subsequent fall of the sea to its present level, it might
be argued that this theory would most readily explain the coincidence
in level between the marine drifts of Macclesfield Forest, Frondeg,
Moel Tryfan, and the Three-Rock Mountain, especially when we
take into account the great distance between the first- and last-
named localities, and the comparatively very small vertical distance
between the highest known shelly drifts and the present sea-level
(about 700 to 1). It would likewise account for variations in the
rate of submergence, by attributing the variations to changes in the
rate of circumpolar liquidation, resulting from changes in tem-
perature. Against the application of this theory to the district
under consideration, we must take into account the differences in
level between different parts of the land as it stood when the above
marine drifts were deposited, and as it now stands. These dif-
ferences would seem to indicate horizontal inequalities in the rate at
which the land emerged, as might be expected on considering the
extent of the submerged area. Thus the level of the greatest
height reached by the chalk in Ireland (as Professor Hull tells me)
nowhere exceeds 900 feet or 1000 feet. But at the time when
chalk flints were transported to Moel Tryfan the chalk in Ireland
must have reached to about 1350 feet above the present sea-level.
The greatest height to which Eskdale granite extends is 1286 feet ;
but at the time when when this granite was transported to Frondeg,
it must, in situ, have reached to atleast 1400 feet. Ihave ventured
to make these few brief remarks in conclusion with the view of
stimulating to further inquiry on the subject, and partly because IL
have reason to believe that so eminent an authority as Dr. Darwin
is now inclined to the opinion that many of the apparent changes
of level in the land were caused by changes of level in the sea.
SUPPLEMENTARY NOTES.
During the present month (April, 1881), having gone over the
ground described in this paper a fourth time, I am able to furnish
the following additional details:—On going south along the west
side of the axial north-and-south ridge of Minera mountain, I saw
numerous large and small angular stones (Carboniferous grit, sand-
stone, and quartzose conglomerate); but I could find few or no
rounded stones, excepting among the felstone erratics, which must
have come from the west. After crossing the ridge and going in a
S.E. direction down the eastern slope of the mountain, I arrived at a
point nearly half a mile north of Krwau. Here it may be necessary
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS. 367
to remark that though rounded stones in drift may often be seen in
preok-channels and on roadsides, where the ground is flat, I have
not examined any hillock or small mound which did not show signs
of its being composed of rounded gravel and sand. Besides the tour
hillocks with gravel-pits (in one of which I found shell-fragments)
near Mountain Lodge, during my last visit I counted ten which
evidently consisted of drifts similar to deposits on our present sea-
coasts. North of a brook which joins another brook near Krwau,
I saw three rather low mounds with surface-excavations sufficient
to show that they consisted of rounded gravel and stratified sand.
The furthest north of the mounds was quite 1300 feet above the
sea-level. While continuing my journey in a northerly direction,
I saw many well-rounded stones in drift exposed in a brook-channel
about 1350 feet above the sea. On descending towards a house
called Braich (1031 feet above the sea, as I have been informed by
Fig. 3.—Section of Drift-deposits between Braich and the Summit
of the Ridge, Frondeg, Denbighshire. (The levels, with the
exception of the lowest and highest, are approximate.)
W. E
A ; 3
¢ % ai 3 2 2
o o A ao a a
Ss set a 4 Ss] 9 &
rs > O) ises ae - en
wt Ye) » ° a v me) Be
Se & Ge a Gro, ais) a8 =
Do tant a ao +O a
i ae Sun Teva ae iG
S oO = oe) 045 3
5c ete Romer” ole 3
Ex Peat covering clay 3 By IB Gis) Bios a
5 with angular stones. oO a S) Oo Q
f | 4 i '
i t 1 1 I
1 ! , , 1 1
fo ; i} } ! 1 i
D af 1 1 ' 1 {
Tp i I \ 1 l I i
ee ~. “ry ~ 1 1 ! 1 : '
=e SSS df A 4 eS 1 I 1 1 {
—a... nos Lee
a ~ Pein, 1
ee ON | FER OUS c al ' f
—_____ —_ >_—. Rl T AND S Fas
aoe
the Director of the Ordnance Survey), I encountered a knoll (fig. 3)
about 1250 feet, showing the marks of a now disused gravel-pit,
containing many rounded stones and sand. The shelly gravel-pit
(described in the paper) lies between the above knoll and Braich.
North of the latter there are three gravel hillocks between
1100 feet and 1150 feet. West of the house called Cae-mynydd
there is a rather large hillock showing the remains of old gravel-
pits. West and N.W. of it there are several large mounds (the
highest nearly 1400 feet above the sea), the character of which is
doubtful; but in one of them several small excavations show a
mixture of rounded and angular gravel. A similar kind of drift
may be traced nearly to the north end of the mountain. I had pre-
viously seen Kskdale granite only in the shape of small pebbles ;
but on this occasion I stumbled on two large blocks, one N.W. of
Cae-mynydd, and the other associated with numerous millstone-
grit blocks on the summit of the axial ridge (about a mile west of
368 D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS.
Braich) at a height of about 1450 feet above the sea (fig. 3), which
proved a submergence of the mountain to at least that extent.
During a fourth visit to the Mountain-Lodge district (above
Ruabon) I found that higher up than the extensive area of rounded
gravel there was an interval of angular detritus, above which (and
near to the summit of the mountain-range) at a height of about
1550 feet, there was a mass of gravel as much rounded as that in
which I found shells at a lower level. Gravel more or less rounded
reappeared on the west side of the mountain at nearly the same
height.
During a third visit to Moel Tryfan (June 1881) I found that
several new sections had been exposed, in which a close inspection
showed that the edges of the slaty laminse were not continuously
curved, though the broken-off chips were arranged along more or
less curved lines which inclined from the N.W.
I ought to mention that, in the observations which have resulted
in this paper, | was again assisted by the Committee of the Govern-
ment Fund for Scientific Research.
Discussion.
The President, in inviting discussion, spoke of the great value of
Mr. Mackintosh’s paper.
Mr. DuRance spoke of the laborious manner in which Mr.
Mackintosh had carried out his work, and thought that he had dene
much to refute the theory of a universal ice-cap overwhelming every
thing. He said that he had examined some of the Molluscan fragments
in Ireland, some of which were, indeed, scratched; but others, he
thought, could only have been deposited during a submergence. He
thought that the positive evidence in favour of submergence must
overpower mere theory. As you ascend the slope of the Halkin
mountain from the river Dee, you pass first over Glacial Drift con-
taining erratics from the Lake district and south of Scotland ; mm the
lower part a Boulder-clay resting on sands with Mollusca; but higher
up the hill there is a different drift, local in character, and contain-
ing only North-Wales rocks.
Mr. UssHrr inquired if the Moel-Tryfan deposit abutted against
higher ground, as then the subaerial débris shed upon the beach
might have been mixed with it, and a local reversal of lamin pro-
duced by the impact of an iceberg.
Prof. Bonny said that he thought the facts. brought forward by
Mr. Mackintosh would give a death-blow to the idea that the Mol-
lusca had been brought up hill by glaciers. He doubted, however,
whether the creep of the mingled sand and clays down hill would
not account for the bending of the slate-edges better than the
srounding of an iceberg; for would not that bend them up hill? and
how would it ground on the lee side of the hill? If terraces were
formed by the rising of the sea due to a polar ice-cap, then they
should not be uniform in level, but rise along circles of longitude
towards the pole.
D. MACKINTOSH ON HIGH-LEVEL MARINE DRIFTS, 369
Dr. Hicks thought that no theory could be founded on the special
direction of the slaty curvatures, as he had seen them in all direc-
tions. He asked if a glacier crossing Ireland along a north-west
direction might not dam the sea up, so as to partially overwhelm
Wales. He did not understand how the erratics could arrive at
exactly the same points both from Ireland and the Solway.
Mr. Macxintosu, in reply, said that he thought that a grounding
iceberg might, if raised first up hill, then slip slightly down hill,
and so bend the edges of the slaty lamine. To Dr. Hicks he replied
that the currents in the sea were far from being necessarily parallel.
370 C. PARKINSON ON THE ISLE-OF-WIGHT
27. Upprr Greensanp and Canoritic Mart, Istz or Wicut.
By C. Parkinson, Esq., F.G.S. (Read March 23, 1881.)
AurHouer the Isle-of-Wight Greensands have been well explored by
eminent geologists, such as Fitton, Mantell, Ibbetson, and Saxby,
there yet remains ample work for paleontologists in the classifica-
tion of the fauna characteristic of each horizon. Hitherto the
fossils from different zones have not been clearly separated, the
collections from the Malm rock being mixed with those of the
upper cherts and rags, and the Chloritic Marl with both. In form-
ing a collection illustrative of the above series, it has been the writer’s
aim to divide every zone and to define the extent of each.
At the base of the section a band of chert nodules is indicated,
measuring 2 feet, which is possibly the true junction of Gault and
Greensand, although in the Memoir on the Geological Survey of the
Isle of Wight 50 feet of micaceous sands below this pomt have been
included in the Greensand ; this has also been done more recently
by Dr. C. Barrois, of Lille. It was from this section, exposed on
the St.-Lawrence beach, that Captain Saxby procured a species of
Crayfish ; and a second specimen has been found within the last
eighteen months in the same locality. The importance of this
horizon has apparently been overlooked ; for quite recently a further
valuable addition has been made to the fauna by the discovery of a
Chelonian previously unknown to paleontologists. From Captain
Saxby’s day to the present time the locality has been neglected.
About a year ago Mr. Mark Norman, a well-known local geologist,
noticed a huge boulder of this blue chert lymg exposed to the wash
of the tide; it had certain indications on the exterior which led
him to examine the whole surface with care; there were, in fact,
the perforations of bone clearly shown. With great care the
hard matrix was chiselled out, revealing portions of the carapace
and rib-bones of a Turtle of the family Paludinosa. The specimen
is now in the Natural-History Museum, South Kensington ; and
through the courtesy of Prof. Owen I am enabled to give the
following notes, abridged from a description kindly made by him.
It is referred to the
Order CHELONIA.
Fam. PALupINosa.
Genus PLastremMys, Owen.
PLASTREMYS LATA, Owen.
A new genus and species of freshwater Tortoise from the Isle-
of-Wight Greensand, remarkable for its breadth in proportion to
length. In this character it approaches nearest to the Tertiary
Emys levis; but the transverse dimension is not eked out, as in that
species, by the accessory plastral plates, and the plastral portions of
the marginal plates are respectively less broad in Plastremys, and
UPPER GREENSAND AND CHLORITIC MARL. ort
allow a large relative proportion of the plastron to the under-
surface of the portable dwelling.
The constituents of the plastron are in normal number, as in the
typical Emydians; there are no accessory pieces interspersed
between the hyo- and hypo-sternals, as in the Wealden genus
Pleurosternon.
The precise measurements, together with figures and minute
description, will be published shortly. In the meantime the fact of
the discovery of a freshwater Tortoise in the Upper Greensand is of
interest, throwing additional light on the conditions of life in that
epoch, and involving either the proximity of a continent or the
remains of island faunas distributed in the marine deposits.
The Crayfish obtained by Saxby, figured in Prof. Bell’s Mono-
graph of the Crustacea, and the Chelonian found more recently by
Mr. Norman, evidently prove that more thorough investigations
among these chert rocks might result in further important additions
to the Greensand fauna.
The next 20 feet of compact red sand are for the most part
unfossiliferous ; or rather the organic remains have been nearly
obliterated. It is harder in texture than the succeeding 4 feet.
Without any other lithological change than hardness, we suddenly
come to a zone in which well-preserved casts of Mollusca abound,
differing, as will be noted, from the Upper Cherts and Rags in a
remarkable manner. At the base of this (that is, 20 feet from the
lowest chert nodules) an Ammonite occurs, which, so far as I can
discover, has not been described. Two specimens found by Capt.
Ibbetson are now in the Jermyn-Street Museum, unnamed; a third
is now in the Natural-History Museum, South Kensington, in
my Isle-of-Wight collection, recently purchased by the Museum
authorities. It has been placed provisionally by Mr. Etheridge as
a species between A. auwritus, and A. rostratus ; though I think it
will be found to differ from both sufficiently to rank as a new
species. It is invariably of the same size, from 23 to 3 inches in
diameter, and remarkably thin for its size, not having the pro-
minent tubereles of A. auritus or the sharply defined chambers of
A. rostratus. At the back the markings are alternate, more resem-
bling the Gault species A. interruptus. Dr. Wright, of Cheltenham,
was unable to identify my specimen with any species known to him.
Immediately above, though never intermixed, the following
fossils are found :—
Ammunites auritus, Sow.
rostratus, Sow.
Trigonia aliformis, Park.
T. ornata, D’ Orb.
vicaryana, Lyc.
Panopea plicata, Sow.
mandibula, D’ Ord.
Plicatula pectinoides, Sow.
Ostrea canaliculata, D’ Orb.
Pecten orbicularis, Sow.
Cardium Gentianum, Sow.
Area carinata, Sow.
Cucullea glabra, Park.
fibrosa, Sow.
Natica sp.
Cinulia sp.
Vermicularia econeava, Sow.
Rhynchonella latissima, Dav.
Terebratula biplicata, Broch,
Modiola sp.
Serpula antiquata, Sow.
aie C. PARKINSON ON THE ISLE-OF-WIGHT
And suddenly as this horizon appears, so it disappears, the succeed-
ing 32 feet being identical with the sands below in lithological cha-
racter, with the exception of being less hard and gradually getting
lighter in colour as we follow it up the section. Organic remains are
few and far between, Holaster levis (on the authority of Dr. Wright,
F.R.S.) being the only distinctive fossil. Up to this point the
fauna may fairly be said to belong to the same epoch ; and collections
from the lower division should be kept separate from those from the
upper cherts and rags, which we now come to, and which indicate
different conditions of life. The red sands give place to alternate
bands of hard chert and coarse greensands (vide section). In the
6 feet of inferior building-stone A. rostratus attains its greatest
development, and casts of large Nautili are common. This is divided
from the building-freestone (which hardens on exposure to the at-
mosphere) by one foot of blue chert, having another chert band on
the top little else but a mass of sponge-spicules imbedded in siliceous
matrix. In the next bed of Greensand Pecten orbicularis is plentiful,
though by no means confined to that band. Pecten cnterstriatus is
not uncommon on the exposed surface of the succeeding Chert band,
and species of Zima in other bands which could not be identified
with certainty. The fossils may not all be confined to the various
beds. Pecten asper, Lamk., never occurs in the Isle of Wight in
these Cherts or Greensands; it is confined to a bed of phosphatic
nodules in the Chloritic Marl, but is probably derived from older
rocks, being in most cases much crushed and broken.
The following fossils are from the Upper Chert and Rag beds :—
Siphonia pyriformis, Park. Exogyra conica, Sow.
Nautilus elegans, Sow. Ostrea frons, Park.
sp. Lima aspera, Sow.
Lima, large sp., strong ribs. Ostrea vesiculosa, Sow.
Pecten, 14 ribs, (Galliennei ?). Cucullea glabra, Park.
Cardium sp. Pecten orbicularis, Sow.
Holaster sp. interstriatus, Lezon.
Ammonites rostratus, Sow. — }-costatus, Sow.
Clathraria Lyellii, Manz. sp.
The Cycadeous plant Clathraria Lyell was first noted by
Mantell, who obtained his specimen from a quarryman in Bon-
church; it was not obtained from the Chalk Marl, but from the
Greensand Rags. A second specimen of this rare fossil was found
at Steephill, near Ventnor, last winter, 10 feet below the Chloritic
Marl, in the same bed as the former one. The remains consist of the
top of the stem surrounded by petioles or leaf-stalks, the leaves them-
selves being either shed or decayed. It has usually been considered
a plant of Wealden age. If, however, island floras and faunas can be
shown to have existed during the formation of the Greensand strata,
oth Chelonia and remains of plant-life are at once accounted for.
The Chloritic or Glauconitic Marl, lying immediately over the
Greensand, may be traced along the escarpment of the Undercliff,
from Blackgang to Luccombe, cropping out finally near Culver Chiff.
It varies in thickness from 6 to 7 feet, and may be divided into two
UPPER GREENSAND AND CHLORITIC MARL. 373
beds, the lower 23 feet, with few fossils, divided by a layer of phos-
phatic nodules (with broken Pecten asper) from the upper 33 feet,
which are rich in fossil remains. The best sections are at Ventnor-
station quarries and below Old Park, St. Lawrence.
A. Fossils derived, in phosphate.
Ammonites varians, Sow. Solarium ornatum, Sow.
Pleurotomaria sp. Pecten asper, Lamk.
Hamites sp. Venus sp.
A. curyatus, Sow. | Cinulia sp.
Rynchonella Grasiana, D’ Orb. Gibbula levistriata, Seel.
B. Fossils slightly phosphatic.
Ammonites Coupei, Brongn. Emarginula sp.
varians, Sow. Terebratulina striata, Wahl.
—— Mantelli, Sow. biplicata, Sow.
navicularis, Mant. semiglobosa, Sow.
eurvatus, Mant. Plicatula pectinoides, Sow.
sp. Rbynchonella Grasiana, D’ Orb.
Hamites attenuatus, Sow. Pecten orbicularis, Sow.
Scaphites zqualis, Sow. (very Beaveri, Sow.
rare). interstriatus, Leym.
Nautilus elegans, Sow. Terebratula pectita, Sow.
expansus, Sow. Discoidea subuculus, Leske.
Turrilites Morrisii, Sharpe. Micrabacia coronula, Goldf.
tuberculatus, Bose. Cidaris vesiculosa, Goldf.
—— Wiestii, Sharpe, Vermicularia concava, Sow.
This Chloritic or Glauconitic Marl has caused considerable con-
troversy as to its origin. I think the presence of phosphatic nodules
between the two beds, together with crushed Pecten asper in great
numbers, has not been sufficiently noticed. This would suggest a
violent and sudden destruction in the phosphate bed, while in the
upper 32 feet nearly all the Mollusca remain fairly periect, and
Pecten asper is not found.
Mr. A.J. Jukes-Browne suggested the name of “ zone of Scaphites
equalis”’ for this marl ; but as it is extremely rare to find a specimen
of this Scaphites lower than the Chalk Marl, I would propose ‘zone
of Turrilites Morrisii,” which is peculiar to the Chloritic Marl.
The best sections and measurements of the Isle-of-Wight Upper
Greensands were made as far back as 1849 by the late Capt. Ibbetsor.
These, together with measurements lately made by Dr. C. Barrois, of
Lille, I prefix to my own section.
Capt. Isprrtson. Coes a
1. Zone of chert and rag with P. orbicularis, P. 5-costatus ... 15 O
Pepurlomerate OF chert and Tag ........-.0:..sseseecnneeceosonee 40
PEE AMM HECSLONC' (5.05... )-ccoctccecacaseccedseecosscacsccencaccees Bye
pempbbecensoneameulayers Of TAG... 2.2... ieee ee ce eeet vows eteewees [kG
2 EE ibd, ela 0 eae ee is ek ee a ee 16:8
6. Mammillary rag, sandy boulders with phosphate of lime.. 1 6
“2, (LOL 922d) so AG Reese coe 6 8
PEP MEAS THANE 2 52 css cs- sec co-escneccccnscecceesseesontevees 3 0
2. DLE 200 i a a eee 40 0
103 6
2 3.G.S. No.147. 2Q¢
374. C. PARKINSON ON THE ISLE-OF-WIGHT
Dr. Barrols. ft.
: in.
= i) Chioritie marl yin case eee 8 0
<3 D Greensand andichert) .-.ns-.ce.s--cceesesee oe 26 0
- |C Greensand, phosphatic nodules ............ 6 6
A
g
8 es Yellow sands with bands.................065. 13 0
= A Micaceous, glauconite sands ............... 117 0
N
170 6
(The order of this section is reversed for uniformity.)
Section of Upper Greensand and Chioritic Marl, St. Lawrence
and Ventnor, Isle of Wight.
{ Chloritic marl 33 feet (fossils list B, slightly phos-
| phatic).
G feet. nee cence Hard phosphatic nodules, with crushed Pecten asper.
| 23 feet compact, darker grains: few fossils, mostly
\ derived.
( Blue chert bands ; casts of Cardium sp.
Coarse greensand ; ; casts of Cucullea glabra, and
| Holaster sp. Chert.
94 feet Greensand: Ostrea, Cucullea, Arca.
“| } —_—___| Chert: Lima sp.
| Chert : Pecten interstriatus.
Greensands: P. orbicularis.
—-—] Chert with sponge-spicula imbedded
(————-| 5 feet freestone, used for building-purposes: casts of
| Nautilus pseudoelegans, N. elegans.
Chert, with phosphatic nodules.
14 feet... 1 6 feet inferior building-stone: casts of Nauwzilz.
| Amm. rostratus here attains its greatest development.
; ————| Blue chert.
| 32 feet yellowish-red sandstones, varying in hardness.
Organic remains few.
Holaster levis (on the authority of Dr. Wright).
| .| Zone of Amm. inflatus, Sow. A. awritus, A. rostratus,
5G feet d Panopea, Cucullea, Arca, Trigonia. About 4 feet.
“| ) —____| Compact red sands.
—-—| Species of Ammonites undetermined, between A, rostra-
tus and A. awritus.
Compact red rock, harder than the above, 20 feet,
unfossiliferous.
D2 feeb. le eewset Nace Blue rag, fossiliferous. Astaciform Crustacea, Che-
—__- —— lonia; passing into Gault sands.
102 feet...
It will be found that the three measurements agree very nearly.
Dr. Barrois includes the 50 feet of sands below the lowest two-foot
bed of chert nodules, as has been done in the Geological Survey
Memoir. In Dr. Barrois’s hasty visit to the Isle of Wight, I think
he inaccurately divided the zone of P. asper and A. inflatus, both of
which are confined to extremely narrow limits. With regard to
Capt. Ibbetson’s measurements, I think the zone of fossiliferous
malm is placed too high up; otherwise the section is very accurate.
In conclusion, I would call attention to the necessity for greater
care in separating the fossils of each zone. Thus Pecten asper, P.
UPPER GREENSAND AND CHLORITIC MARL. SMe)
eretosus, P. Beaveri, Lima sp., P. Gallienner(?) may eventually
be found to characterize different zones, while the entire fauna of
the malm rock is different from that of the chert and rag beds.
I would propose, also, that the 50 feet of sands included in the
Upper Greensand by Mr. Bristow, and more recently by Dr. Barrois,
should be referred to the Gault, taking the well-marked band of
chert boulders with Chelonia &c. as the true base of the Upper
Greensand.
I also suggest, with some diffidence, that remains of island floras
and faunas exist in the marine deposits of those Greensands, as
evidenced by a freshwater Tortoise and Cycadeous plants, the former
authoritatively stated by Prof. Owen to be a freshwater reptile,
while the leaf-stalks and stems of tropical plants speak for them-
selves.
Dr. Barrois’s division of the Upper Greensand into two zones
is misleading, as the fossils are confined to such narrow limits. I
would suggest, in place of this, several zones in the upper cherts
identified by characteristic Pectinide, which are the best-preserved
of the Mollusca, the fauna of the Malm rock being clearly separated
from that of the Rag.
Mr. J ukes-Browne’s zone of Scaphites equals is imaccurate.
20 feet higher up in the Chalk Marl S. equalis is abundant; in the
Chloritic it is hardly ever found. Turrilites Morrisii is, on the
other hand, characteristic of this horizon.
The band of phosphatic nodules with crushed Pecten asper de-
serves attention. ‘This species of Pecten is certainly not properly
a Chloritic-Marl fossil; yet 1t only occurs in the peculiarly crushed
state in this formation; it is never found in the Greensand proper
in the Isle of Wight.
Discussion.
Mr. H. G. Forpuam stated that between Ballard Hole and Pun-
field Cove the phosphatic nodules are scattered through the Chloritic
Marl, and not confined to its base, and that no broken shells of
Pecten asper occur at that point. He further remarked that the
author gave the thickness of the Chloritic Marl as 6 feet, 7. ¢. greater
than previous authors.
The Presipent stated that the new Ammonite mentioned by the
author seemed to be intermediate between A. rostratus and A.
awritus, but nearer to the former. Pecten asper had not previously
been noticed above the Upper Greensand. He referred to the great
yalue of Dr. Barrois’s labours in connexion with the English Chalk.
Rev. J. F. Braxe thought that the beds with Ammonites inflatus
belonged to the Upper Gault, and not to the Greensand.
Mr. J. Srarxte GarpneR thought that, as species of Pecten and
Lima have often a long range, their value for characterizing horizons
in the Cretaceous was doubtful.
Mr. De Rance stated that Pecten asper in Dorsetshire never
occurs above the Greensand. He agreed with Mr. Blak» in re-
garding the zone of Ammonites wnflatus as Upper Gault.
Zc 2
376 E. W. WILLETT ON A MAMMALIAN JAW FROM
28. Norss on a Mammarian Jaw from the PurBeck Bups at Swanace,
Dorset. By Evear W. Wituerr, B.A. With an Introduction
by Henry Witxert, Esq., F.G.8. (Read May 25, 1881.)
(Communicated by the President.)
Inrropuctory Remarks. By Henry Wittert, Esq., F.GS.
The rarity of the fossil remains of mammals in Mesozoic strata
is a paleontological fact so well known to the Members of thig
Society, that it would be superfluous in me to do more than
allude to it.
All needful information will be found in the exhaustive. mono-
graph (by one of the greatest living authorities on comparative
anatomy, Prof. Owen) published in 1871 by the Paleontographical
Society. From it I gather that in 1828 Mr. Broderip first dis-
covered Didelphys in the Stonesfield-Slate quarry.
In 1858 the teeth of Mrcrolestes were discovered by Mr. Moore
in a breccia of Rheetic bone-bed and limestone filling a fissure in
the Mountain Limestone at Frome, in Somersetshire.
In 1864 my friend Prof. Dawkins discovered a worn molar of a
Marsupial mammal in the Rheetic beds at Watchet, in Somerset-
shire, called by him Hypsiprimnopsis rheticus (Microlestes rhe-
ticus). But it was to the personal energy and perseverance of _
Samuel Beckles, Esq., F.R.S., that science was indebted for the
discovery of the great variety of these interesting fossils, the de-
scription of which occupies the largest portion of Prof. Owen’s
work (loc. cit.). My own imagination was excited by a popular
account of Mr. Beckles’s labours, written about 1858 by the late
lamented Canon Kingsley; and the desire for further discovery
caused me to pay several visits to the ‘‘ Dirt-beds” at Swanage, in
the hope of making further additions to the catalogue of Mam-
malian remains. fuddven I must have spent slbnee ther many
hours in search on several oecasions, aided at times by local quarry-
men, I could never succeed; but in 1878, having learnt that.
Mr. Beckles had been obliged, unwillingly and prematurely, to
abandon his researches at a posits which seemed rich in promise, I
obtained leave from the Earl of Eldon, on certain reasonable con-
ditions, to renew the inquiry at the point left by Mr. Beckles. The
year 1879. was too wet and stormy to allow me to carry out my
intention in so perilous a position.
There are two so-called “ Dirt-beds ” in the Purbecks of Durdle-
ston Bay, Swanage. The lower one can be readily examined from
the shore, as it rises at varying angles from beneath the sea-level
until it is lost in the débris and turf above.
The upper dirt-bed, which also crops out at a similar angle, is
less distinctly defined, until we reach a point about two thirds of
the way up the cliff, just below the commodious refreshment-room
THE PURBECK BEDS AT SWANAGE, DORSET. Ta
erected on the summit of the cliff; and it was at this point (at
which Mr. Beckles, hoping to resume his labours, had purposely cast
down a large protecting accumulation of debris) that our attack
was finally made ; in the summer of last year, 1880.
I must here render my tribute of thanks to my able coadjutor,
Mr. Henry Keeping, of Cambridge, for the skill with which he
directed the work, at no. little peril to those engaged in it.
We commenced operations by scarping down the overhanging
strata for a depth of 40 feet, laying bare an area about 13 feet by
10. This upper “ dirt-bed” is of varying thickness, from 2 to
10 inches. It seems to have been a silt, filing up hollows and irre-
eularities in the surface of the stratum immediately below it.
Aided by those earnest geologists Prof. Dawkins of Manchester,
Mr. Charles Potter of Liverpool, Mr. Griffith of Cambridge, and
several members of my own family, the area was most carefully
broken up and examined. The research occupied ten days; and
although we found several teeth and jaws (hereafter to be described),
it was a fortuitous blow of the hammer of a local quarry-man that
laid bare the interesting specimen about to be described.
The-time of the meeting has already been trespassed upon too
long by these preliminary remarks. I hope on some future occa-
sion to supplement them by a further description of the fossils dis-
covered, a more ample account of the probable conditions under
which the deposits were formed, and the reasons which explain
. the rarity of discovery rather than the paucity in number of the
Mammalian remains.
With the jaw of Triconodon, and in the same bed, were found
rocodilian remains (Zheriosuchus pusillus, Ni annosuchus g gracilidens,
and Nuthetes destructor), with other Mammalian and Reptilan
fragments not easily determinable. There appears to be a single
tooth of Theriosuchus amongst the fragments, but whether of 7’.
pusilus is doubtful.
Ir will be remembered that rather more than twenty years ago
extensive explorations were undertaken by Mr. Beckles, F.R.S., at
Swanage, in search of Mammalian remains, and that he succeeded
in unearthing some dozen new genera, including altogether sixteen
new species of Mesozoic mammals. These fossils consisted prin-
cipally of mandibles more or less broken, the only other bones
found being portions of the upper jaw.
In the early summer of this year the permission of. Lord Eldon
was obtained to renew the search in Durdleston Bay, Swanage ; and
although this search was not followed by such brilliant results as
in Mr. Beckles’s case, it cannot be said to have been to no purpose,
since a very good Mammalian jaw was obtained.
The specimen consists of the larger part of a right mandibular
ramus, of which the condyle, the upper border of the coronoid
process, and the symphysial end anterior to the second premolar
are wanting. Six teeth altogether are preserved in svtu, and, with
378 E. W. WILLETT ON A MAMMALIAN JAW FROM
the exception of the foremost, one are quite perfect. The genus to
which the specimen belongs is Zriconodon, Owen; but it differs
Fig. Lower jaw of Triconodon mordax, Owen, from Swanage.
Nat. size.
from those described by Prof. Owen in his Monograph on the
Mesozoic Mammalia* in the fact that it has four teeth having the
form of true molars, all those previously found (eleven or twelve in
number) having each only three true molars, ‘a reduction rare in
the Marsupial order,” to which these mammals are usually ascribed.
It may be noticed here that the nearly allied genus T'riacanthodon
has four true molars, but that the teeth now under consideration
differ from those of this last-named genus in the following im-
portant details :—The fourth premolar of Triacanthodon approaches
the triconodont or true molar type; and the apex of this tooth
reaches only to half the height of the main cone of the preceding
premolar, whereas the main cone of the fourth premolar of the
new jaw is by far the largest of the three cones, and is rather
longer than the corresponding cone of the preceding tooth ; again,
no hinder talon is found in any of the four molars of Trzacanthodon,
while it is well marked here on each tooth.
Of the six teeth preserved, four are, judging by form, true molars,
and two are premolars, each of which is implanted by two roots;
the two sockets for the next premolar are also plainly visible.
The crowns of both the premolars consist of a principal sub-
compressed cone, with a small and low anterior basal cusp, and a
large and higher posterior one followed by a rudimentary talon ;
of the two the anterior tooth is rather the smaller.
All the true molars agree with the description .of the type
specimen of Prof. Owen in being ‘“ subcompressed, antero-pos-
teriorly extended, and divided into three nearly equal cones in the
same longitudinal line, the middle cone being very little larger than
the front or hind cone; further, there is no cingulum on the outer
side of the crown, but at the posterior margin of the posterior cone a
rudimentary talon is feebly marked off by a short vertical indent
from the rest of the surface of that cone.” The first of the true
* «Monograph of the Fossil Mammalia of the Mesozoic Formations,’ by
Prof. Owen, F.R.S. D.C Ll. Printed for the Palzontographical Society.
London 1871
THE PURBECK BEDS AT SWANAGE, DORSET. 379
molars is rather smaller than the others; and, as in the type speci-
men alluded to above (plate iii. figs. 7, 7 4, loc. cit.), the base of
the coronoid process hides part of the last tooth. Prof. Owen con-
siders that this character may indicate that the jaw described by
him belonged to an individual not quite fully grown. Assuming
such to be the case, the fourth molar in the present specimen would
point to a mature animal, though, for a similar reason, to one not
yet adult. In point of size, the last premolar and the three anterior
molars agree as nearly as possible with the corresponding teeth in
the type specimen of 7’riconodon mordax.
The question, therefore, to be settled is, Does the new specimen
belong to this last-mentioned genus and species or not?
Prot. Flower, who has kindly examined it, and compared it with
those found by Mr. Beckles, which are now in the British Museum,
thinks, on the whole, that it may probably be referred to this species,
and ingeniously suggests two hypotheses to account for the extra
tooth of true molar form. ‘They are as follows :—
As is well known, the deciduous teeth of the Marsupials, to
which group the Mesozoic mammals have hitherto been assigned,
consist of a single tooth on either side, the tooth which replaces
this deciduous one being the last premolar. Assuming, then, that
this tooth is still in setu, and is represented by the third tooth,
counting from the symphysis, the dental formula will bep.m. 4
m. 3, which agrees with the type specimen of T'riconodon mordax
in the British Museum ; and the first hypothesis is that the jaw
belonged to a younger individual than any previously found, with
the single milk-tooth in position.
The second hypothesis is to assume that all the teeth preserved
belonged to the permanent set, when the dental formula will be
p-m.3,m.4. In this case the four molars agree in number with
those found in the adults of all recent Marsupials, and indicate a
more fully matured specimen than any hitherto discovered.
A third hypothesis is to assume that it belongs to an altogether
distinct species; but this, considering the close resemblance to
Triconodon mordax, appears hardly necessary.
The lower border of the ramus is, in its present condition, nearly
straight; but it has been much crushed, and when recent was, with-
out doubt, slightly curved.
A small outlet of the dental canal opens under the foremost root
of the third premolar (the first which is preserved); and there are
traces of one, if not of two, other outlets anterior to this.
The total length of the jaw is 13 inch.
Discussion.
Mr. H. Witterr said that he hoped the specimen would be accepted
by the authorities of the School of Mines, and placed in the collec-
tion there.
Prof. Duncan spoke of the importance of the communication and
the thoroughness which it showed. The jaw was a highly developed
380 ON A MAMMALIAN JAW FROM SWANAGE, DORSET.
one; and had not the marsupial nature been suggested, it might
have been considered to belong to the Insectivora ; probably, how-
ever, it was an insectivorous marsupial. But was it so certain that
the jaw belonged to a marsupial of the present type? It was
strange also that these remains of marsupials had, at present, only
been found in Europe. He was under the impression that the
Australian marsupial fauna was not very ancient.
Mr. Cuartesworte said the history of the discovery of mammalian
life in Britain was interesting. It had a important bearing on
evolution. The explanation of the occurrence of lower jaws only was
well known; but it was difficult to explain the disappearance of the
phragmocones of Belemnites: also in Kast Anglia only teeth, antlers,
and astragali of Cervz were found ; other bones were wanting.
Mr. E. Witter said that mammalian remains had been recently
found in great numbers in America, on about the same horizon, and
that from them the discoverer, Prof. Marsh, was led to believe that
all Mesozoic mammals belonged to a more generalized type than do
the marsupials which at present exist.
ane
ey
ye
yeh a ee
An vas, fink on
yal
aiid
mM piaey:
¥ i
5
®
¢
&
a
.
;
y
¢
Quart, Journ. Geol. Soc Vel XXXVI PLXIX.
A.S Foord lth JURASSIC DIATOPORIDAS
G. R. VINE ON THE FAMILY DIASTOPORID&. 381
29. Further Notes on the Family Diastovoripe, Busk. Species from
the Lias and Oottrr. By Grorer Rozert Vine, Esq. (Com-
municated by Prof. P. Marrmy Duncan, M.B. Lond., F.R.S.,
F.G.S.) (Read January 19, 1881.)
[Puate XTX.]
Since my first paper, ‘‘A Review of the Family Diastoporide for
the purpose of Classification” *, was written, a very important book
has been published, namely ‘A History of British Marine Polyzoa,’
by the Rev. Thomas Hincks?. In this work the classification
adopted by Prof. Busk in his Monograph of the Fossil Polyzoa of
the Crag, 1859, and also in his british-Museum Catalogue,
part ii. Cyclostomata, 1875, is set aside for one that J have little
hesitation in saying will prove to be far more valuable to the
working student. Instead of separating Diastopora, and making
it the type of a family, Mr. Hincks places this genus with others in
his second group of the Cyclostomata, which he calls Incrustata,
DOrb. The family name which he adopts is Fam. IL. Tubuliporide,
which includes the genera
Stomatopora, Bronn. | Entalophora, Lamouroux.
Tubualipora, Lamarck. Diastopora, Lamouroux (pt.).
Idmonea, Lamourouc.
Seeing that I have already committed myself to Prof. Busk’s
arrangement, it is impossible for me now to retreat; and, with this
explanation, | must be excused for still adhering to the famuy name
I used at first ?.
In his remarks on the Cyclostomata, Mr. Hincks says :—‘ Sim-
plicity isin the highest degree characteristic of the group; the cells
are universally tubular; the polypide is without complexity of
structure, and has a small number of tentacles; all appendicular
organs are wanting” §. In another place he says:—‘ In classi-
fying the Cyclostomata we have to base our divisions mainly on
habit or mode of growth, on the plan according to which the
zocecia are aggregated together into colonies; the simplicity and
general similarity of the cell throughout the tribe leave no other
course open to us. We have to deal with very uniform struc-
tural elements very variously combined; and the modes of com-
bination chiefly supply us with the bases of our system. Under
* Quart. Journ. Geol. Soc. vol. xxxvi. p. 856 (August 1880).
Tt Van Voorst: 1880.
t Of the two evils I choose the least. To call my paper “ Further Notes on
the Tubuliporide” would be to commit myself to remarks on the other genera,
which at present I have no intention of doing; and the retention of the family
name Diastoporidz, Busk, may have its special advantages.
§ Brit. Marine Polyzoa, Introduction, p. exxy.
382 G. R. VINE ON THE FAMILY DIASTOPORIDZ.
these circumstances we may not expcct very strongly marked
boundary lines” *.
The family Tubuliporide, Hincks, is thus defined :—“‘ Zoarium
entirely adherent, or more or less free and erect, multiform, often
linear, or flabellate, or lobate, sometimes cylindrical ; Zowcia tubu-
lar, disposed in contiguous series, or in single lines; Owciwm an
inflation of the surface of the zoarium at certain points, or a
modified cell” +.
These further Notes have reference to the Diastopore found in
the English Lias and Oolite, and are the results of a very careful
study of material kindly and liberally placed at my disposal by two
good local workers, Mr. KE. A. Walford, of Banbury, and Mr. F. D.
Longe, F.G.8., of Cheltenham. Whilst I was engaged in the study
was continually perplexed with the ever-varying modes of growth
of what may be considered to be true Diastopore. ‘To fix many of
these forms under the descriptions already given by authors is
indeed impossible; or to call them, arbitrarily, ‘ species” or
‘“‘ varieties ” would give a false idea of their significance. The
wisest course to adopt is to call them ‘‘types;” and in giving them
specific names I have kept this suggestion constantly before me.
Between the Liassic and Oolitic forms very little variation is per-
ceptible if we select groups of the same or similar habit. If, as in
the Inferior Oolite, for instance, we take the three or four different
types, and try to correlate them under one specific name, the varietal
or typical divergency is at once apparent. In this paper I have
directed the attention of the paleontologist more particularly to
these typical forms; and it remains now for local workers to mark
the differences well, and then, by a rigid and philosophical scrutiny,
to try and ascertain whether any of these varietal types creep gra-
dually from one into the other. The doing of this as it ought to be
done depends on whether material for the scrutiny is accessible to
the student ; and besides the material, patience is needed to follow
out a set design to its conclusion. To take away the stigma so con-
tinually repeated to our disadvantage, “ the imperfection of the
geological record,” work done in the direction indicated must be
attempted, even if it be imperfect; but, after going over only a
small portion of the labours of two local workers, I believe it to be
possible to carry out the design to perfection, or nearly so, if keen
eyes and willing hands are engaged in the task.
I am not aware that previously to the labours of Prof. Quenstedt
the attention of the paleontologist had ever been directed to Liassic
Polyzoa. In his great work, ‘Der Jura,’ many Liassic fossils are
described and figured, and amongst others we have figured and
described the earliest known Mesozoic Diastopora. Quenstedt
names it D.lasica; and he says of it, “ One usually recogn
the primary cell; at first a rapid increase occurs; but the poly-
zoarlium soon divides itself into two groups, draws itself back, and
* Brit. Mar. Polyzoa, vol. i. p. 425.
t Ubid. vol. 1. p: 424
G. R. VINE ON THE FAMILY DIASTOPORID®. 383
completes a perfect circle” *. He further says, D. liasica “ occurs
so abundantly, and precisely on shells of the Jurensis zone, that you
can often identify your horizon from it.” ‘The specimen he figures
is found on Ammonites jurensis.
Jules Haime‘, in correlating Berenicea striata, says that this
species was discovered by M. Terquem in the Lias of Valiére. He
says :—‘ D. lrasica, Quenstedt, Handb. der Petrefact. p. 637, pl. lvi.
fig. 10, “is closely related to this species: it begins in the same
manner with a plate in the shape of a fan; but it branches out more
on the outside.”’
Dumortier, in his ‘ Paleontological Studies of the Jurassic De-
posits of the Basin of the Rhone,’ recognizes another species, as he
calls it, in the fourth part of the Superior Lias. This he names
D. crussolensis ; and the only distinguishing feature between this
and D. liasica is *‘ that it grows thicker than the last, and the form
of the colony is more circular” $.
In Mr. E. A. Walford’s pamphlet on some Upper and Middle Lias
beds in the neighbourhood of Banbury §, the author relies upon
Quenstedt’s description for the identification of his specimens found
in the zone of Amm. spinatus, and also in the transition-bed, on
corals and shells.
In the best work on Oolitic Polyzoa that I have yet met with,
‘Description of the Fossil Bryozoa of the Jurassic Formation’ ||,
Jules Haime divides his typical Diastoporide ito two groups, the
Berenicece and the Diastopore. The incrusting forms treated of as
Diastopore in this paper belong to the first group of Haime. His
species are:—B. diluviana, Lam., a common form of the Great
Oolite; B. Archiaci, Haime; B. microstoma, Mich.; and B. lucensis,
Haime. Both of these last are found in the Bradford Clay and the
Great Oolite, very beautiful species with very characteristic cells.
The Diastopore of Haime belong to the Foliaceous group. Another
paper, by Prof. D. Brauns{[, contains some very valuable in-
formation on both the foliaceous (especially lea) and incrusting
Diastoporide.
Mr. Walford has placed in my hands, for description or study, the
whole of his local fossil Polyzoa; and so inadequately have the
species been described and figured, that, for scientific purposes, the
labours of these eminent paleontologists are almost useless. In
giving the Liassic species a new name, I have had regard more
particularly to its typical character than to any thing else. In this
Liassic type I recognize a family likeness to later fossil and more
recent Stomatopore ; and it will be advantageous to science to draw
attention to the fact.
* “Der Jura,’ pp. 279-292, fig. 1, tab. 40.
t+ Bryoz. fossiles de la form. Jurass., in Mém. Soc. Géol. de France, 1854.
{ Dumortier, /. c. p. 226, pl. 48. figs. 11, 12.
§ Proceedings of the Warwickshire Naturalists’ and Archeological Club, 1878.
| Loe. cit.
{| Zeitschr. d. deutschen geolog. Gesellsch. 1879.
384 G. R. VINE ON THE FAMILY DIASTOPORIDA.
1. Drastopora stoMatToporiIpEs, mihi. Plate XIX. figs. 1-10.
? D. liasica, Quenstedt, Handb. der Petref. p. 637, pl. lvi. fig. 10.
? D. crussolensis, Dumortier, Paleont. Studies, p. 226, pl. xlviii.
figs. 10 & 12.
Zoariwum subcircular or orbicular, sometimes indefinite in its mode
of growth, forming small isolated patches on shells or corals, varying
in breadth from one and a half to three lines. Zowcia arranged
linearly, or nearly so, long and slender tubes, many of them
wrinkled or surface-roughened, and adherent by their whole length ;
orifice, when perfect, oval, rarely circular. Primary zocecia either
very excentric in the larger colonies, or proximal in the smaller
ones, Which soon become excentric as the colonial growth increases.
Oeca rare, when present pyriform, involving at lees two of the
cells. Zocecial tubes very faintly punctate.
Hab. On Amm. cornucopie, Up. Lias, Bloxham; on Cardinia
hybrida, Sow., Appleton ; and on fornia Victoria, Mid. Lias,
zone of Amm. Henleyr, Cherrington, Oxfordshire ; Sup. Lias, Crussol,
Dumortier ; on Amm. jurensis, in zone of ditto, Southern Germany,
Quenstedt. ‘ Deeper than this,” says Quenstedt, “ I have never
found it.”’
A careful study of the figures given will convey to the paleeon-
tologist a very fair idea of the character of this very early Mesozoic
type of Diastopora. Unlike any of the palzeozoic types, it seems to
be persistent, so far as the character of the cell is to be relied upon,
high up into the Oolitic series, and, but for the peculiarity of its
maar, might be recognized in the Stomatepora deastoporides, Norman, —
and the Tubulipora lobulata, Hassall*. Indeed, of the first of these
species Mr. Hincks says “ that it is the largest of British Stoma-
topore, and has very much the look of Diastopora;” and of the
other species, ‘“‘I can see no sufficient ground for placing Tubuli-
pora and Diastopora in separate families; the two genera are nearly
related, and have many common characters.” He said this without
being aware of the existence of the forms now figured and described,
which are in every sense confirmatory of the justness of his family
arrangement.
In the Oolitic series, beginning with the lowest beds—the Pea-
we recognize altogether different types,
not widely separated, but even on the same blocks. ‘These types
belong to the foliaceous as well as to the crustaceous forms; and
where to draw the line between the two it is difficult to say. In
some few cases the boundary lines are broken down; and one at least
of the typical Diastopore pass from the crustaceous into the foli-
aceous form by a series of quiet gradations. Mr. Longe has given
more attention to these forms than I have; and his remarks on these
peculiar species may be referred to for exact informationy. After
* Figures and description in Hincks’s Brit. Polyzoa, vol. i. pp. 434 & 444,
pls. 61 & 63.
t Geological Magazine, January 1881.
G. R. VINE ON THE FAMILY DIASTOPORID®. 385
a careful study of the crustaceous forms from several horizons,
ranging from the Pea-Grit to the Coral Rag, I can detect at least
three types that have not been specially noticed, so far as I am
aware, by previous authors. ‘hey may, and I have not the least
doubt that they have. been, casually identified; but that is all.
They deserve, however, more than a passing notice, because some of
these types, when they pass into the Bradford Clay and the Forest
Marble, delicately preserved on branches of Terebellaria and frag-
ments of broken shell, assume an altogether different character.
Some of them are beautifully papyraceous ; others appear to have a
kind of basal lamina extending slightly beyond their circumference,
a character I have never observed in the Inferior-Oolite species.
The papyraceous species of the Lower Oolite are also deserving
of closer study than I can possibly give to them. Such work belongs
rather to local students than to me. They, too, may study the
types as they pass from one stratum to another; and in so doing, I
would recommend them to mark the beginnings of the divergences,
and the boundary lines of each of the four types given; and by
doing so they will aid the paleontologist in classifying the evolu-
tionary stages of a most important genus.
2. DrastopoRaA VENTRICOSA, mihi. Plate XIX. figs. 15-17.
Zoarium adnate, discoid in the earlier stages of growth, of most
irregular outline in its later stages. Zowcia produced and partially
free in the centre, gradually depressed towards the margin; tubes
slightly bent and swelling towards the orifice, which causes a con-
striction of the circular or subcircular mouth; cells well separated,
the proximal ends heing immersed in the zoarium. Occia very
largely developed, sometimes round the margin, at other times indis-
eriminately all over the colony, involving two or three cells or only
a considerable swelling of a single tube. In the best-preserved spe-
cimens the cells and also portions of the ocecia are finely punctate.
Hab. Ona weathered and partially smoothed pebble (No. 5),
Inferior Oolite, Pea-Grit, Cheltenham: Mr. Longe’s Cabinet. On
drift wood, Chipping Norton, lowest beds, Great Oolite: Mr.
Walford’s cabinet. Good specimens also in Museum of Practical
Geology, Jermyn Street.
This species, or type, is a very peculiar one, well deserving especial
study. I have it from several localitics, ranging from the Pea-Grit
to the Great Oolite. The specimen in Mr. Walford’s cabinet
contains innumerable colonies piled up very irregularly round a
piece of water-logged coniferous wood of Oolitic age.. The wood
was originally large; but the broken fragment submitted to me for
examination was about three inches long, and from half to three
quarters of an inch in diameter. The incrustation of the wood,
made up wholly of colonies of Diastopora, varies in thickness from
a quarter to half an inch, the margins of the newer colonies
eradually becoming compressed into the general mass through
successive stages of growth. The ventricose swellings are not so
typical in this specimen as in the more beautiful specimens from
386 G. R. VINE ON THE FAMILY DIASTOPORIDA.
the Pea-Grit series (Mr. Longe’s cabinet). One colony is five lines
by four; and the ocecia are well developed, for there are no fewer
than from 25 to 27 swellings in various stages of development ; and
it is from this specimen that the drawings (Plate XIX.) are taken.
Measured across the cell-mouths, there are about six (or varying
from five to seven) cells to a line. Three ocecia occupy about the
same space. ‘The earliest stages of colonial growth are disks with
free cells, flabelliform at later stages, ultimately presenting the
appearance of one continuous mass of immersed cells. On the
broken edge of a fragment of Mr. Walford’s specimen I can count
from twenty to thirty layers, representing successive colonial
growths.
It may be that some at least of the specimens of this type are the
Berenicea diluviana of authors, and the Diastopora verrucosa of
Milne-Edwards. Berenicea Archiaci, Haime, is closely related to
this species ; but the cells, and also the occia as figured by Haime*,
are not so characteristic of our own Oolitic series as D. veniricosa.
3. DrIAsToPoRA ooLiTicaA, mihi. Plate XIX. figs. 11-14.
Zoarium circular or nearly so, completely adnate, and varying in
size from one to three lines in diameter either way. Zocwcia short
and bulging near the distal, gradually contracting towards the
proximal end ; orifice variously shaped, the lower margin, in some
cases, slightly mucronate (?); primary cell excentric. Central
zocecia partially raised, becoming gradually depressed towards the
margin. Oacia? Tubes faintly punctured, and no “ adventitious
tubules.”
Range from the Pea-Grit to the Great Oolite.
Cabinets: (from several localities) my own; Miss Gatty’s, Kidling-
ton, Oxon; Mr. Longe’s, very rich, from Pea-Grit; and also from
Mr. Walford’s ; Museum of Practical Geology (several specimens on
shells).
Pa On stones and shells, forming small disk-like patches, more
frequently isolated than clustering.
This delicate little species is the most abundant of the Oolitic
Diastopore. From its peculiar habit specimens are generally referred
by collectors to the D. obelia of Busk; and in my early identifica-
tions I was inclined to place it as a variety (var. oolztica) of that
species. After drawing and carefully working out the type I soon
found this to be impossible. The general habit is different ; the cells
are more closely packed, and their shapes are altogether different ;
and, above all, there is in none of the specimens I have examined
any indication of ‘‘ adventitious tubules.” Judging from Manzoni’
figure t, which he refers to Berenicea striata, J. Haimet, a doubt na-
turally suggested itself when correcting the proof of my first paper$
as to whether some specimens of this type may be referred to
Haime’s species. There seems to be no identity either with that or
* Bryozoa Jurassic Form. pl. ix. fig. 11.
+ Fig. 79, Bryozoa of the Pliocene of Castrocaro.
¢ Reuss, Die Bryoz. des braunen Jura von Balin, &e.
§ Quart. Journ. Geol. Soc. vol. xxxvi. p. 357, note.
G. R. VINE ON THE FAMILY DIASTOPORIDA. 387
Busk’s D. obelia. D. oolitica is a very characteristic type, especially
of the Pea-Grit Series, in the Cheltenham district at least.
Another type, not the least important of the whole group, is a
most peculiar one. In general habit and mode of growth it seems
to be a true Diastopora ; but it must be looked upon more as a pas-
sage form than as a constant one in all its characters. The type of the
cells, when slightly worn, approaches nearer to that of the Paleozoic
Ceramopore than to any Mesozoic Diastopore; but in the more perfect
cell the largely developed peristome is unlike any thing in the more
ancient or the more recent Diastoporide. If this be a true passage-
form, rather than a constant one, the tendency is toward the Pus-
tulopora-subverticellata type*. In this type the cells are connate ;
but in the one under consideration only some few of the cells are
connate; the great majority are “ separated pores,” as in ordinary
Diastopore. My diagnosis is made from both the younger and older
growths of several colonies ; and the description may be relied upon,
however the species may be placed in the future. In the Pea-Grit
Series the cells have a very bold outline, with interspaces (in some
places) between cell and cell. In one specimen from Chipping
Norton the cells have a Lepralia-like growth, the colonies being
semicircular and piled one upon another; and some of the cells are
so immersed that only the peristome can be seen. In naming this
“type” or “species,” I desire to preserve a generic name, though
the genus itself is now merged in that of Entalophora and Spi-
ropora.
4, Drastopora cRIcoporaA, mihi. Plate XIX. figs. 18-25.
Zoarium adnate, forming small and large irregular patches, some-
times self-attached, at other times incrusting other species of
Polyzoa. In the early stages of growth the colony has a bicircular
or oval outline; in its later stages the growth is most irregular.
Zoecia short and stunted tubes, very coarsely punctate; orifice
ring-like, with a largely developed peristome. Primary zoccium
inconspicuous, being deeply immersed, giving off to the right and
left secondary zocecia, which in their turn give off others. .The
after colonial growth is thus early directed to two opposite points ;
ultimately the proximal cells unite below the primary cell, so that
it in time becomes centric or excentric. Owcia?
Range from Pea-Grit to Great Oolite.
Cabinets: several very fine specimens of this type are in the cases
of the Museum of Practical Geology, Jermyn Street; Mr. Longe’s,
Mr. Walford’s, and Mr. Windus’s.
Hab. Chiefly on water-worn stones and broken shells.
I have had very great difficulty in describing this type, more
particularly on account of its peculiar preservation. One colony on
Mr. Longe’s specimens (block 6) is very well preserved in its earliest
“stages ; and from this specimen most of the figures are drawn. The
natural size is shown at fig. 18, and is about three lines at its widest
* See Busk’s ‘ Crag Polyzoa,’ pl. xviii. fig. 1, right-hand specimen.
388 G. R. VINE ON THE FAMILY DIASTOPORID A.
part. In fig. 19'(an enlargement of a portion of the same colony) the —
tendency of the cells to the right and to the left is shown; the other
figures are enlargements of special cells to show the ring-like cha-
racter of the mouth and peristome. ‘There is another colony on the
back of the same slab; but this is very much worn, and the cell-
mouths are somewhat angular. The largest colony is on block 9*;
and it is a very interesting study. ‘This block is a piece of coarse
Oolitic Limestone, much worn by attrition; and, besides many
Serpule, it contains on its surface several colonies of Polyzoa.
Fig. 25 is a magnified portion of a colony of D. cricopora adherent
to a colony of Hlea(?), or one of its nearest allies, the one almost
wholly enveloping the other. In the fragment figured the different
characters of the two fossils areshown. The under one of the Elea (?)
type has all the cells in one plane, the walls of each cell so closely
connected as to leave no interspaces. The normal orifice of the
cell seems to be of a subcircular character ; when slightly worn it is
large and circular, unlike any of the cell-mouths figured by Busk
in his ‘Crag Polyzoa’ as Mesenteripora, which seems to have been
used as a synonym ~ of Hlea foliacea (D. foliacea, Lamx.). Manzoni
also figures t a “ Diastopora” ? having a habit somewhat similar to
this, which he calls D. expansa, Manz. ; but the aperture is normally
circular with a well-developed peristome. This flat adherent type
of the Inferior Oolite becomes (so Mr. Longe informs me) foliaceous
in its after stages; but whether it ever becomes really leaf-like with
cells on both sides I cannot, as yet, satisfy myself. I have no desire,
however, to put this type under the genus Diastopora. ‘The other
incrusting form is a marginal portion of D. cricopora, having many
of the characters of the group, but with cells altogether at variance
with the general build of the true Drastopora-cell.
The genus Diastopora has been, and is, in many instances, very
much abused ; and before proceeding with these studies it may be as
well to define and limit the genus. Lamouroux used two terms which
have come into general use—the one Berenicea, and the other Dias-
topora. Under these two names many divergent forms have been
placed, so that to some extent Berenicea and Diastopora are synony-
mous terms, the term Berenicea being used for one section of the
Diastoporid and Diastopora for another section. In subdividing the
foliaceous Cyclostomata, Milne-Edwards formed two great groups,
‘« distinguished,” says Busk, ‘‘ by the character that in the one the
ubes are almost wholly immersed, and in the other partially free.”
To the former group Milne-Edwards applied the appellation ‘ Dras-
TOPORES,” and to the latter that of “ Tuputrporss.” ‘ This division is
natural ; but it seems convenient that it should be carried still further ;
* These numbers refer to the specimens as numbered in Mr. Longe’s cabinet.
It would be a good thing to have the types preserved in some public museum,
so that they could be accessible to future students. Whenever I could, I have
referred to specimens so preserved.
+t D’Orb., Pal. Frane. terr. Crét. (p. 808).
t Briozoi di Castrocaro, tav. vi. f. 83.
G. R. VINE ON THE FAMILY DIASTOPORID®. 389
and in the doing of this... no better classification can be adopted
than that suggested by the same author, viz. into 1. Diastopores
simples; 2. D. enveloppantes ; 3. D. bisérialaires. I propose, there-
fore, to term the simple Diastopore of Milne-Edwards Diastopora, the
enveloping or laminated forms Berenicea, and the biserial Mesenterz-
pora’”*, This arrangement Mr. Busk follows in his ‘ Crag Polyzoa.’
But Mesenteripora is placed as a genus of the Tubuliporide, whereas
in the Museum Catalogue, part 111. Cyclostomata, it is placed as a genus
of the Diastoporide. This I have no objection to, because it is only
those who have gone over the same ground who can possibly know
what difficulties there are to encounter in classifying the species
under discussion. The differences, however, between Mr. Busk and
Mr. Hincks* are very striking on this point. In the ‘ Catalogue of
Cyclostomata,’ Mesenteripora (a foliaceous form of the Diastoporide)
is included in the Famity ; whereas in ‘ British Marine Polyzoa’ the
foliaceous forms are included in the genus Diastopora. ‘This I entirely
object to, on account of the confusion it is sure to create when we
are dealing with Mesozoic forms. With this exception Diastopora,
in the sense in which I have used it, may be defined as follows :—
“ Zoarium adnate and crustaceous, usually discoid or flabellate,
less commonly irregular in form. Zowcia tubular, with an elliptical
or subcircular orifice, crowded, longitudinally arranged, in great
part immersed.”
The foliaceous species will have to be separately dealt with; and
I think it very unwise to use the term Berenicea, as defined by
Lamouroux, for other than Paleozoic species. IRPf Berenicea is used
for Paleozoic and Oolitic species indifferently, simply because the
*‘corallum incrusts foreign bodies ” and is “ composed of a thin cal-
careous base” t, confusion will be sure to follow, for the simple
reason that the characters of the Paleozoic and Oolitic species
are altogether different. The Ceramopore and Berenicee of the
Paleozoic rocks are not typical Diastopore.
There now remain for investigation the Chalk- and Greensand-
forms; and these I would gladly revise if Members would help me
by the loan of material for this purpose. Some of the species
catalogued are undoubtedly Drastopore; others are not Diasto-
pore in the restricted sense used by me in this paper.
My thanks are due to kind friends who have assisted me with
material for the writing of this paper—to Mr. Walford for supply-
ing me with extracts and tracings from Dumortier and Prof. Braun,
and to Mr. J. D. Longe, F.G.S., for the loan of specimens from the
‘Inferior Oolite. I also tender my thanks to Mr. R. Etheridge,
F.R.8., and to Mr. E. T .Newton, F.G.S., for allowing me to examine
the specimens in the Museum of Practical Geology.
* Crag Polyzoa, p. 109.
+ British Marine Polyzoa, p. 457.
t M‘Coy, Brit. Pal. Foss. p. 44.
Q.J.G.8. No. 147. 2D
Figs.
Figs.
Figs.
Figs.
G. R. VINE ON THE FAMILY DIASTOPORIDA,
EXPLANATION OF PLATE XIx.
1-10. Diastopora stomatoporides, Vine.
1, 2. Natural size of two different colonies.
3,4, '7. Enlarged respectively about 10, and 15 diameters, to show the
disposition and character of the cells.
5, 6. X 25 diam., showing the elongated character of cells, together with
the rugose markings on some.
8. x 50 diam.
9. xX 30 diam.
10. Aperture of cell, X 50 times, to show the true Elea-foliacea (Dia-
stopora, Lamx.) type of peristome; from colony. Fig. 4. As aboye.
(Compare Berenicea striata, Haime, pl. vii. fig. 8, a,b, ‘ Foss. Bryozoa
of the Jurassic Formation.’) .
11-14. Diastopora oolitica, Vine.
11. Natural size of colony.
12. x about 8diam. There is much variation in this type; but it has
generally a circular habit, as depicted.
13. X about 33 diam.
14. x about 50 diam.
15-17. Diastopora ventricosa, Vine.
15. Natural size of colony. This also varies as to size of colony.
16. x 25 times, showing the disposition of the ocecial ‘“‘ goneecia,” Hincks,
in the different parts of the colony.
17. X about 50 diam.
18-25. Diastopora cricopora, Vine.
18. Natural size of colony from which the typeisdrawn. The specimens
in the School of Mines vary considerably.
19. Portion of colony, enlarged in the direction of line I, fig. 18, to show —
the disposition of the partially immersed cells.
20-22. x 25 times, giving a fair illustration of the ornamentation of the
cells.
23, 24. x 75 times.
25. Two separate colonies: the uppermost, D. ericopora (marginal edge),
incrusting Elea foliacea, Lamx. |
Discussion.
The PresipENT bore witness to the great value of the author’s
study of this group of microscopic organisms.
Prof. Srrtey stated that his study of the Polyzoa had led him to
conclude that many of the supposed generic differences were mere
accidents of age and growth. He thought that Mr. Vine’s paper
was
a valuable addition to science. He doubted the wisdom of
inventing wholly new names for previously described species, as had
been done in one instance by the author.
@uart:
Frank Rutley del. A.S Foord hth
Journ.Geol. Soc Vol. XXXVI, PL XX
Vie Os BOCKS OF MONTANA UES.
N
F. RUITLEY ON THE VITREOUS ROCKS OF MONTANA, U.S.A. 391
‘30. The Microscopic Coaracters of the VirrEous Rocks of Montana,
U.S.A. By Frank Rurtzy, Esqg., F.G.8. Woth an APPENDIX
by James Eccrus, Esq., F.G.S. (Read April 6, 1881.)
[Prats XX. ]
THE specimens which have supplied the material for this paper were
collected by Mr. James Eccles during a tour in Montana. They
present so many interesting points of structure that a description of
their microscopic characters:‘may prove acceptable to those who are
engaged in the study of British vitreous and devitrified rocks.
Among the latter we have already found that certain structural
peculiarities may still be clearly recognized, notwithstanding the
changes which have led to their more or less complete devitrification.
Through these changes, once vitreous rocks assume the character of
felstones; and as it is highly probable that many of our ancient
‘“‘felstones ” and ‘* hornstones” were once vitreous, it becomes im-
portant that we should note every structural peculiarity in glassy
rocks of recent or late geological age which have undergone little or
no change subsequent to their solidification. By doing this we are
training our eyes to recognize similar structures in the devitrified
obsidians, perlites, and pitchstones which ran over what are pro-
bably the earliest land-surfaces of which we have any trace.
Zirkel, in his ‘ Microscopic Petrography of the 40th Parallel N.,’
has described a large number of structures met with in the districts
surveyed by Messrs. King, Hague, Emmons, and other members of
the U.S. Government Survey ; and it is to him we owe much of our
knowledge concerning these minute structures. In this country the
researches of Prof. Bonney and Mr. Allport have also served to in-
erease the interest which rocks of this class will always possess.
The more carefully and patiently we study the unaltered examples,
the better shall we be able to deal with the questions which concern
their older and no longer vitreous representatives ; while researches
upon artificial slags or glasses formed under known conditions, and
modified by various known causes, either during or subsequent to
solidification, will lend additional help in explaining minute struc-
tural peculiarities which still remain to be worked out.
The following is a description of the microscopic characters of
ten of the most interesting specimens (which may be regarded as
fairly typical of the whole series) collected by Mr. Eccles in this
district. In each case the letter M precedes the description of the
microscopic characters.
No. 1. Yellowstone district. Black obsidian.
A black and perfectly vitreous rock, speckled with rather sparsely
_ disseminated small greyish-white flecks, which are generally imper-
fectly developed felspar crystals.
M. In this section it is transparent and colourless, and is a re-
markably homogeneous glass. The porphyritic crystals (which are
2p 2
392 F. RUTLEY ON THE MICROSCOPIC CHARACTERS
not very numerous) are, in some if not in all cases, orthoclase.
Some are perfectly developed; others present the most ragged and
irregular boundaries, as in the accompanying figure (fig. 1). In -
Fig. 1.—Felspar Crystal in Obsidian (black), from the Yellowstone
i District. (Magnified 55 times, crossed Nicols.)
“aa - ate
: ASN ow, &,
this instance the spicular projections are sufficiently long and
delicate to completely invalidate the supposition that the crystal
is a broken fragment, and to render it absolutely certain that it
has been developed during the cooling and solidification of the rock
in which it occurs, or else that it is a partially dissolved crystal.
This is an important piece of evidence, because less irregularly
bounded imperfect crystals might often be erroneously regarded as
included fragments taken up by and enveloped within the lava.
Moreover it is interesting to see how, in such a remarkably homo-
geneous matrix, this crystal, if aborted, fails to assume the globular
form, rounded at the angles, which is so common in the porphyritic
crystals developed in most vitreous rocks. Under an amplification
of 300 or 400 diameters numerous clear granules and opaque tri-
chites are visible, as shown in fig. 1, Pl. XX.; and there are many.
small objects which may be elongated gas-pores ; but, as they mostly
pass diagonally through the section from the upper to the lower
surface, it 1s not easy in all cases to ascertain their true character,
owing to the impossibility of bringing them into focus throughout
their entire length. Those which coincide with the planes of section
certainly appear to be elongated, and sometimes tortuous, gas-pores.
The trichites are sometimes straight, sometimes curved, and frequently
form stellate groups. 7
No. 2. Yellowstone district. Obsidian. ots3
Reddish-brown or Indian-red coloured rock, with some dark brown
or black streaks and mottling, opaque, except in thin sections.
Bright vitreous or slightly resinous lustre, and imperfect conchoidal
fracture.
M. It is seen bytransmitted light (fig. 2, Pl. XX.)to consist of delicate
bands or strings of a clear yellow or orange-colour, with here and there
_ afew bluish-black or grey strings. The material lying between these
coloured strings, which are very closely packed, is a colourless or
OF THE VITREOUS ROCKS OF MONTANA, U.S.A. 393
almost colourless glass. The yellow fibres depolarize in all azimuths
except those coimciding with the directions of the principal sections
of the crossed Nicols. ‘There is therefore a marked optical difference
between the yellow and the colourless bands, the latter being per-
fectly isotropic*. The generally parallel disposition of the bands
imparts an appearance to the magnified section which very closely
resembles the structure seen in a longitudinal section of wood; and
this resemblance is further heightened by the deflection of the bands
around small porphyritic crystals and fragments of quartz, which
may be likened to little knots in wood. Although the greater por-
tion of the preparation appears dark between crossed Nicols when
the general direction of the bands is parallel with one or other of
the Nicol-sections, still the deflected bands around the porphyritic
erystals transmit a strong brownish-yellow light, because they do
not, in this position, coincide with either of the Nicol-sections, so
that around each brightly depolarizing porphyritic crystal there are
also depolarizing fringes resembling smoothly-combed tresses of hair.
Some of the porphyritic quartz-crystals have irregular creeks of glass
passing into them, in some cases the yellow fibres being mixed with
the included colourless glass, thus clearly showing that these quartz-
erystals were actually developed within the rock prior to or during
its solidification. The preparation also shows numerous dark opaque
granules and a few dark sections, apparently of minute octohedra,
which are opaque, except at their margins, where they feebly trans-
‘mit light; and this imperfect opacity seems to imply that they are
not magnetite. The fine banding in this rock is a most perfect ex-
ample of fluxion-structure.
Representatives of this class of rock, similar in structure, but
more or less devitrified, are to be found among the lavas of early
Paleozoic age in North Wales.
No. 3. Yellowstone district. Black spherulitic obsidian.
A black glassy rock, containing numerous pinkish or pale-grey
spherules irregularly distributed and varying from the size of a pea
downwards to very small dimensions.
M. The section is seen to be traversed by bluish-grey and colourless
bands, the former consisting of streams of microliths (fig. 3, Pl. XX.).
In this banded structure there is no depolarization, showing that the
banding in this case is quite different from that in the red obsidian just
deseribed. The spherules either occur isolated or in little colonies.
Porphyritic felspar crystals occur here and there, and they show a
few glass enclosures.
No. 4. Yellowstone district. Spherulitic-banded obsidian.
A rock consisting of dull dark grey and vitreous black bands,
flecked with white porphyritic crystals of sanidine.
M. The dull bands are seen to consist of radiately crystalline
spherules ; while the deep-black bands visible in the hand-specimens
appear in thin section as clear and colourless glass. In the drawing
* Since this paper was read, I have satisfied myself that the double refraction
in these coloured bands is probably due to strain, a thick bundle of spun glass
exhibiting similar phenomena.
394 F, RUTLEY ON THE MICROSCOPIC CHARACTERS
(fig. 4, Pl. XX.) two portions of one and the same sanidine erystal,
which between crossed Nicols undergo extinction synchronously in
the same azimuth, are separated by spherulitic matter; and this
seems to indicate that the spherules and crystals were probably
developed at the same time. az
No. 5. Yellowstone district. Black porphyritic obsidian.
A black glossy rock, with white porphyritic crystals, some of them
+ inch long. A smoothly-ground surface shows fine, continuous,
greyish, parallel bands and porphyritic erystals in a deep-black
ground-mass. The fractured surfaces of the specimen are very irre-
gular or small conchoidal.
M. The bands are seen to consist of closely aggregated spherules ;
and the surrounding glass is filled with streams of microliths, which
impart a finely banded appearance to it. The porphyritic erystals
lie with their longest axes in the same direction as the bands. One
erystal (part of which is shown in fig. 5, Pl. XX.) is completely sur-
rounded by a border of small spherules; and in another instance a
little crystal lies immediately within a rudely concentric series of
perlitic cracks. The section is fissured in all directions, the cracks
traversing the glassy matrix, the spherulitic bands, and the por-
phyritic crystals; they must therefore have been produced subse-
quently to the formation of those bodies. A few of the porphyritic
crystals in this rock bear a close resemblance to olivine. One
transverse section of a rhombic prism gives an angle of 94°, which
corresponds with the angle in olivine. The face of the section shows
the granulated surface so frequently seen in olivine-sections ; the
angles of the crystal are slightly rounded; and the fringed cracks
which traverse the crystal closely resemble those seen in olivine.
The extinctions, moreover, in this crystal coincide with the directions
of the crystallographic axes, assuming the section to be transverse
toarhombic prism. If this crystal be olivine (as I believe it to be),
we have a curious instance, possibly the only one yet recorded, of
olivine occurring in an obsidian. Zirkel, however, describes the
occurrence of olivine in a trachyte from the top of Whitehead Peak
in the Elkhead mountains, which he says “ presents, beside sanidine,
very many cracked quartzes as large as a pea, hornblende, and augite,
and, what is remarkable, not very numerous but doubtless charac-
teristic half-serpentinized olivines, the sections of which, measuring
as high as 0°75 mm., are visible even to the naked eye in the slides.
The peculiar quartz occurring here is therefore accompanied by a
mineral which has never before been observed in a sanidine rock” *.
No. 6. Yellowstone district. Spherulite rock. .
A pale bluish-grey rock, slightly cellular and with yellowish-brown
stains, with numerous little porphyritic felspar crystals (chiefly
sanidine) and, exceptionally, some roundish grains of quartz. On
a smoothly-cut surface the rock is seen to consist almost wholly of
closely aggregated spherules, with a little dark glassy interstitial
matter. It is, in fact, an obsidian almost completely devitrified by
* “Microscopical Petrography,” p. 159 (U.S. Exploration of the Fortieth
Parallel: Washington, 1876).
OF THE VITREOUS ROCKS OF MONTANA, U.S.A. 395
the development of spherules and small porphyritic crystals, and
may be regarded as a spherulitic condition of sanidine trachyte
or rhyolite.
M. It is seen to consist of a multitude of spherules which possess
a radiating, crystalline, or fibrous structure, and consequently show
dark crosses between crossed Nicols (fig. 6, Pl. XX.). The spherules
vary in diameter from about ;4, inch to extremely minute specks,
when the section appears (in these parts) to pass into a microcrystal-
line condition, apparently identical with felsite. Indeed, from the
microscopic study of this and many other more or less closely allied
rocks, it appears to me desirable to abolish any hard lines of classifica-
tion which have hitherto been drawn between the trachytes, rhyolites,
and felstones. The spherules frequently form continuous and some- ~
what tortuous strings, which, between crossed Nicols, resemble the
chenille put round the bottom of glass shades to exclude dust. The
porphyritic felspars frequently fail to show any definite crystal-
lographic boundaries, and are occasionally penetrated by creeks of
the surrounding substance, which in one or two instances is included
and shut off from the matrix. The porphyritic quartz-grains are
often irregular in outline, and do not appear to have any good fluid
enclosures.
No. 6a. Yellowstone Cafion. Quartz rhyolite.
A pale bluish-grey compact rock, showing delicate wavy fluxion-
bands, which, on a smooth surface, are seen to thin off, seldom being
continuous for more than an inch. Numerous small porphyritic
grains of quartz and a very few crystals of sanidine are also visible.
M. The ground-mass of the rock is seen to be apparently micro-
_ granular, while the bands also show a microcrystalline or crystalline-
granular structure, but very much coarser. It is Just the same tex--
tural difference which is still visible in microscopic sections of our
archean and paleozoic rhyolites. The ground-mass varies in texture
in different parts of the section; and, where finest-grained, it is
studded with little roundish blotches, which seem to depolarize more
strongly, and which appear lighter than the ground-mass when the
Nicols are crossed, and darker when they are set parallel, or when
the section is seen by ordinary transmitted light. When examined
with an amplification of about 250 diameters, these spots seem to be
the result of devitrification; while by employing a quartz plate it
is seen that the ground-mass is partially isotropic, and the doubly
refracting spots appear to become more mixed with isotropic matter
towards their margins. The spots, in fact, resemble segregations of
doubly refracting granules, which impart a sort of spotty mottling
to the ground-mass. The porphyritic quartz-crystals are nearly all
rounded in outline, like those which oceur in quartz-porphyries ; but,
unlike the latter, they seem to contain no fluid lacune. This rock
affords interesting material for the study of devitrification.
No. 66. Lower Geyser basin; is a pale grey or drab rock, with
darker parallel bands. It is a banded spherulite rock, the bands
consisting of small and the remainder of larger spherules. It closely
resembles No. 6, except in the better definition of the bands. The
rock contains some porphyritic felspar crystals.
396 ¥F, RUTLEY ON THE MICROSCOPIC CHARACTERS
No. 7. Quartz rhyolite. Gardiner’s River.
Compact pale bluish-grey rock, containing numerous granules of
quartz and a few crystals of sanidine. A rudely banded structure is
visible on a smoothly cut surface of the specimen.
iM. Shows curiously twisted and gnarled bands which end abruptly
(fig. 7, Pl. XX.). This may, however, bein some instances due to
their being cut off by the upper and lower surfaces of the preparation.
The structure closely resembles the mottling on gun-barrels. in some
of the thicker bands traces of a fibrous crystalline structure, transverse
to the bands, is visible in polarized light ; and this, taken in conjunc-
tion with the frequently looped or annular disposition of the bands,
_may be accepted as evidence that, at all events to some extent, the
general structure of the rock is due to an attempt to develop sphe-
rules, but especially such as have an elongated axis, as in the axiolites
described by Zirkel.
No. 8. Yellowstone district, Lower Geyser basin. Vitreous tuff
(“‘ obsidian sandstone”).
A finely granular rock of a dark or blackish colour, with light
specks. The granules have a vitreous lustre.
M. It is seen to be a tuff composed of small fragments of vitreous
rocks which in most instances show well-marked perlitic. structure
(fig.8, Pl. XX.), and detached crystals and fragments of crystals which
in most cases appear to be sanidine and occasionally plagioclastic
felspar. The transverse sections of some of the former are lozenge-
shaped, the boundaries being faces of the oblique rhombic prism and
giving an angle of about 118°. These fragments of rocks and crystals
are bound together by a cementing material which, in a not very thin
section, appears brown or even absolutely opaque by substage illu-
mination, and reddish brown by reflected ight. It is most likely
limonite. As already mentioned, the section is a rather thick one;
and between crossed Nicols the majority of the spheroidal spaces
enclosed by the perlitic cracks in the rock-fragments exhibit more
or less well-marked depolarization and a dark interference cross.
The cross is sometimes rather irregular or distorted. In some
instances depolarization takes place only along the bounding cracks ;
in others it forms a well-defined zone, the central portion, where the
arms of the cross would intersect, remaining dark and forming an
approximately round spot, as in fig. 2. These phenomena appear
Fig. 2.—Areas of Depolarization from Strain within Perlitic Bodies
én Obsidian Tuff (“* Obsidian Sandstone”), Yellowstone Dastrict.
most distinctly to be the result of strain; for Lommel* remarks,
* “The Nature of Light,’ p. 330 (International Scientific Series, London, 1875).
OF THE VITREOUS ROCKS OF MONTANA, U.S.A. 397
“the double refraction of compressed and suddenly cooled glass is
nevertheless essentially different from that of crystals;” and he
adds that, in order to project the system of rings of a strained glass
disk upon a screen, using Dubosq’s polarizing arrangement, it must
be placed at a point where “ the rays by which it is struck are nearly
parallel, and traverse the plate in the same direction and with the
same length of path. ‘The difference of path which gives rise to the
system of rings can therefore only be due to the fact that the double
refraction, whilst the course of the rays remains unaltered, increases
towards the periphery of the plate. In a crystal, on the contrary,
the double refraction is at all points the same for the same direction
Othe rays”...
Before proceeding another step I wish to place side by side with
this statement an extract from the late Hermann Vogelsang’s ‘ Kry-
stalliten’*. Speaking of some crystallites in a piece of thick glass
from the glass-works at Stolberg, he states that for a certain distance
around these isotropic crystallites the glass exhibits double refrac-
tion, a neutral cross also traversing the anisotropic area. In one
case he noticed a slight disturbance of this cross in the neighbour-
hood of an ellipsoidal body, which seemed to him to indicate that
the strain in this instance was not constant in all directions; and
he states, ‘‘ It is also to be remarked that the glass at the boundary
of the polarization-picture is sometimes traversed by a fissure, a
spheroidally-running cleft. The polarizing action is not thereby
disturbed. Whether these cracks were produced during the cooling
of the glass, or whether they have subsequently been developed in
the splitting-off and grinding of the preparation, | am unable to say.”
If the careful observer, who penned the lines I have just quoted,
had seen the preparation which is now placed before you, I think
that his doubts with regard to the origin of those spheroidal fissures
would have vanished. We have here, I believe, additional confirma-
tion of the views advocated by Professor Bonney, Mr. Allport, Mr.
Cole, and myself with regard to the origin of perlitic structure.
But we have something more. If Vogelsang’s crystallites be em-
bryonic erystals (as I think we may certainly assume that they are),
we have a close relationship between crystallogenesis and perlitic
fission ; and, indeed, in the section to which our attention is now
confined, there are plentiful examples of doubly refracting crystals
which are immediately surrounded by perlitic cracks, but which do
not, save very exceptionally, transgress those boundaries.
In a paper upon a somewhat kindred subjecty I have already
quoted a statement of Bischoff, to the effect that trachytic rocks, in
passing from a vitreous to a crystalline state, undergo a shrinkage
of nearly 10 per cent. of their original bulk. In those few instances
in which a perlitic crack passes through a crystal, there is commonly
another crystal developed by its side, which, with its surrounding
* “Die Krystalliten,’ Bonn, 1875, p. 68. Admirable figures of these crystal-
lites are given in plates ix. and x. of the vbove work.
+ “On some Structures in Obsician,” erlite, and Leucite,” Monthly Micro-
scopical Journal, vol. xv. p- 183.
398 F, RUTLEY ON THE MICROSCOPIC CHARACTERS
crack, may have been formed subsequently to the crystal which is
traversed by that crack. What are we to infer from these crack-
begirt crystals? Surely we have here something lke the contraction
experimentally determined by Bischof in rocks of precisely similar
constitution. The crystal is a constituent of trachyte; it may be
regarded even as a small piece of trachyte developed within obsidian.
The strain upon the surrounding glass, engendered by the formation
of this crystal, is, I have no doubt, the cause of the rupture in the
surrounding glass; and the gape of the fissure is the measure of the
contraction for any one plane. ‘The polarization-figures seen within
the perlitic areas surely, then, bespeak the incipient strain which
heralds the production of the crystal; and I believe that the
rounded boundaries and the curved cracks, so frequently seen within
the angles of olivine and other crystals developed in vitreous rocks,
are but another expression of the laws which crystallization enforces
in a surrounding amorphous mass. In studying these questions we
seem almost to stand upon the threshold of: crystallography; and I
may well close this paper with the hope that the subject may be
taken up by more able hands; for it requires further investigation,
since there are periites in which no apparent relation exists between
the perlitic structure and the porphyritic crystals—as in some of the
perlites of Chemmitz, where even a score of small perlitoids may be
seen to abut against the margin of a single crystal of sanidine or
of magnesian mica. In these rocks we have, indeed, always assumed
that the development of perlitic structure was subsequent to the
formation of the porphyritic crystals, and not approximately syn-
chronous with it, as 1 think has been the case in the materials of
the obsidian tuff just described. In an inquiry of this kind thick
sections, as well as thin ones, should be prepared and examined, ~
and conclusion after conclusion discarded if needful, until the truth
is reached. Indeed, I am not unwilling to believe that some of the
phenomena which we have just discussed may be due to different
operations of one force, or of different forces; and, just as the same
mineral may sometimes be formed by a wet or by a dry process, so
it is possible that similar structures may not always be due to the
same cause.
AppEenvix.— Microscopic Characters of Volcanic Rocks of Montana.
No.9 (the rock from Mount Washburn) is an andesite which seems to
be intermediate in character between the augite- and the hornblende-
andesites, and approximates in mineral constitution to a basalt.
The constituents are chiefly triclinic felspar, augite, hornblende,
magnetite, and vitreous matter.
A little sanidine also appears to be present. The augite and
hornblende crystals generally show a dark border when examined
under the microscope with substage-illumination. By reflected light
these borders appear of a bright rust-red, and are doubtless due to
marginal decomposition of the hornblende and augite. These stains
and granules of peroxide of iron impart a reddish brown-colour to
the rock. The vitreous matter constitutes a considerable proportion
OF THE VITREOUS ROCKS OF MONTANA, U.S.A. 399
of the ground-mass. A little bright green matter is also present,
which appears to occupy irregular vesicles, and which is either green
earth or some closely allied mineral of secondary origin. The angles
of extinction of the felspars seem to indicate that the triclinic ones
are labradorite.
The rock from Tower Falls closely resembles that just described,
except that it contains apparently no augite and more hornblende.
The erystals of the latter mineral are also surrounded by opaque
borders, which are often broad, and consist of an internal zone of
magnetite and an external one of hematite, which appears sharply
defined at its contact with the magnetite. The rock is hornblende
andesite. It is of paler colour than that from Mount Washburn,
the hand-specimen being grey, with minute reddish brown, black,
and white specks *.
APPENDIX.
On the Move of OcctRRENcE of some of the Votcantc Rocks of
Montana, U.S.A. By James Kccrzs, Esq., F.G.S.
Tue yoleanic district of the Yellowstone National Park, from which
I obtained the various rock-specimens referred to in the foregoing
paper, has been already described in detail by Dr. Hayden, Dr. A.
C. Peale, and Prof. Bradley, in the reports of the U.S. Geological
Survey of the Territories for the years 1871 and 1872.
In the autumn of 1878 I had the good fortune to accompany Dr.
Hayden and other members of his survey in some parts of the
district referred to; and although I have no intention of giving a
detailed description of the voleanic phenomena which were observed,
a short notice of the localities whence the specimens were obtained,
and of the general mode of occurrence of the rocks, may be of some
interest as a supplement to Mr. Rutley’s description of their micro-
scopic characters.
The Yellowstone National Park, within which are the head-waters:
of two of the great forks of the Missouri (the Yellowstone river and
the Madison) and of the Snake river (one of the branches of the
Columbia, comprises an area of about 3600 square miles, nearly the
whole of which is covered up by voleanic rocks of great thickness.
There are very few exposures of underlying sedimentary or other
formations; and these are almost entirely limited to the extreme
northern edge of the area. Some fifteen miles south of the southern
boundary the extension of these volcanic rocks is seen to rest upon
the northern spurs of the Teton range of mountains, at which point
the underlying formation has been ascertained by Prof. Bradley to
be of Carboniferous age. On approaching the Park from the south
along the upper valley of the Snake, these volcanic rocks appear to
form an irregular plateau densely covered with forest. From the
point at which we first struck this plateau, as far as the Upper
Geyser basin on the Firehole river (the chief branch of the Madison),
* For the discussion upon this paper see p. 412.
400 J. ECCLES ON THE VOLCANIC ROCKS OF MONTANA, U.S.A.
Fig. 3.—Map of part of the Yellowstone Park.
(Scale about 20 miles to 1 inch.)
q ss A ee
: =—_ ow =e = @ @ @ — - |
TOWER FAULS Ko 4
MOUNT
Mi wasnauRn |
Ane
ba
=
1295 Pap nosnone
awe eee ee ieee ie
is a linear distance of about twenty-five miles, but three days of hard
travelling. The rocks consist entirely of varieties of obsidian and
trachyte, the latter almost invariably being found in great mass
under the former.
The obsidian, though frequent, is somewhat irregularly distri-
buted. It is both black and reddish brown, is occasionally columnar,
and is nearly always porphyritic. The most common form is a coarse,
rapidly weathering variety, containing many crystals of sanidine.
The disintegration of this rock produces some curious fine conglo-
meratic deposits in the old watercourses and river-beds (No. 8).
The trachyte is constant and of very great thickness, and is evi-
dently closely allied to the obsidian. A cliff-section in the Upper
Geyser basin suggests a transition from trachyte to obsidian. (Nos.
4 and 6 were obtained from this section.)
J. ECCLES ON THE VOLCANIC ROCKS OF MONTANA, U.S.A. 401
* East of the Firehole river and across the divide between the
Madison and Yellowstone rivers the section presents the same gene-
ral characters as that between the Snake and the Madison. High
up on the divide the trachytes are light in colour, and there is some
pumice occurring on the surface. On the east of the divide the
obsidian thins away for some distance, but is found again above
the Great Canon of the Yellowstone, where it is capped by fully
300 feet of fine sandstones and shales, probably of Quaternary age,
which have doubtless been deposited by the Yellowstone lake in a
former period of extension. The rocks in this basin, and especially
in the section exposed in the Great Cafion, have been minutely de-
scribed by Drs. Hayden and Peale; and I have nothing to add to
their description. It is sufficient to say that the order and general
character of the rocks is almost precisely the same as in the upper
part of the Madison basin. .
Up to this point the voleanic phenomena had been almost uni-
form. The trachyte-flows, although dipping shghtly here and there
(as much as 20° in the Upper Geyser basin), were approximately
level; and the country through which I had passed seemed to be
quite destitute of any features which I could recognize as vents from
which such an enormous mass could have been poured out. Seven
miles north of the head of the Cafion a change is observable. Mount
Washburn here attains an elevation of from 2500 to 3000 feet above
the trachytes of the Canon, and is a true volcanic cone. The summit is
abroken-down crater; and the lava-flows, which are basaltic (No. 9),
dip away in all directions, and conform generally to the slopes of the
mountain. I found no contact between the basalts and the trachytes
on the southern side of the mountain; but it is quite evident that
the former overlie, and are more recent than, the great mass of tra-
chytic rocks just described.
Descending on the north side of the mountain, the Yellowstone
river was reached again near Tower Falls, a distance of ten miles
from the peak; and here the trachytes are again seen in the river-
section, with columnar basalts resting on them. I «was not sure
whether these basalts had flowed from Mount Washburn or from
some vent on the east side of the Yellowstone; but, compared with
the trachytes, they were comparatively insignificant both in extent
and, except on the mountain itself, in thickness. ‘These basalts had
been poured out before the formation of the present Cation; for the
river here cuts its way through basalt and trachyte nearly 400 feet
deep.
The locality of Gardiner’s river, whence the specimen No. 7 was
obtained, as well as the intervening spaee between this river and
Tower Falls, was passed over most rapidly by me, owing to bad
weather and Indian troubles. The trachyte in this locality resem-
bles strongly that of the Great Canon in mineral character. Although
there is a considerable distance between Tower Falls and Gardiner’s
river where the trachyte does not exist, owing, probably, to denu-
dation, I am inclined to regard this Gardiner’s-river trachyte as
belonging to the great mass of trachytes further south.
402 ON THE VOLCANIC ROCKS OF MONTANA, U.S.A.
EXPLANATION OF PLATE XX.
Vitreous rocks of Montana.
Fig. 1. Black obsidian containing trichites. Yellowstone district. x 250:
2. Red obsidian showing in thin section reddish-yellow bands of glass,
and grains of quartz, ina nearly colourless glass. Yellowstone district.
x 205.
3. Black spherulitic obsidian with bands of microliths and radiately crys-
talline spherules. Yellowstone district. Xx 77. Nicols at 85°.
4. Spherulitic obsidian, consisting of dull dark-greyish and vitreous black
bands, flecked with white glassy porphyritic crystals of sanidine. The
dull bands are composed of radiately crystalline spherules, while the
vitreous bands consist of glass, black in the hand-specimen and colour-
less in thin section. Yellowstone district. x 25,
5. Black porphyritic obsidian with spherulitic bands. The drawing shows
part of a section of one of the porphyritic crystals of sanidine, which
is surrounded by an isolated girdle of small spherules. Yellowstone
district. x 18.
6. Yellowish grey spherulite rock with small porphyritic crystals of sani-
dine. Yellowstone. x 32. Crossed Nicols.
7. Rhyolite with peculiar Damascene structure and grains of quartz.
Between crossed Nicols it is seen to have a microcrystalline structure
throughout. Gardiner’s River. x 55.
8. “Obsidian sandstone,” a finely granular blackish tuff, composed of
angular grains of vitreous rocks of different appearance, the majority
being perlitic, others showing merely microlithie streaks, but all pro-
bably derived from approximately the same source and representing
the disintegration and cementing in place of vitreous rocks. The
drawing shows part of one of the perlitic fragments, in which, between
crossed Nicols, an interference-cross is seen in the centres of some of
the perlitic spheroids, similar to the crosses seen under similar circum-
stances in artificially stramed or compressed glass. In the lower part
of the field a crystal of triclinic felspar is shown. Lower Geyser basin,
Yellowstone district. x18. Nicols at 85°.
Note.— Except when otherwise stated, the drawings have been made by ordi-
nary transmitted lght.
Quart.Journ.Geol. Soc. Vol XXXVIT PL XXL
Frank Rutley del. A.S Foord lth
Mirtern Brosimp.
WELSH LAVAS OF LOWER SILURIAN AGE.
ON DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 403
31. On the Microscopic Structure of Drvirrirrep Rocks from
BEeppDGELERT and Snownon ; with an Appendix on the ERUPTIVE
Rocxs of Skomer Istanp. By Franx Rourrzy, Esq., F.G.S.
’ (Read April 6, 1881.)
[Puate XXI.|
THz specimen from the south side of the Capel Curig road, about 4 mile
from Beddgelert, which was collected by Mr. George G. Butler*, and
which he kindly placed at my disposal, is a rather dark greenish-
grey rock, spotted with pale greenish-grey spherules, some of which
are over + inch in diameter, and which, besides occurring isolated
and in approximately spherical forms, have also coalesced, forming
bands from 4 inch to nearly 1 inch in breadth. On a smoothly cut
surface they afford, by their pale tint, a strong contrast to the dark
matrix. The isolated spherules and spherulitic bands are shown in
fig. 3 (Pl. XXI.) as they appear when magnified about 6 diameters.
A thin section, when examined between crossed Nicols, is seen to
be studded all over with small doubly refracting specks. By ordi-
nary transmitted light, and under a power of 25 diameters, a marked
difference is visible in the microscopic characters of the spherules
and the matrix, the former being almost colourless, save for a few
pale greenish flecks, which become more closely aggregated at the
margins of the spherules, forming a somewhat darker border, while
the matrix appears to consist of a closely matted or granulated deep-
green substance resembling chlorite, through which are interspersed
a great number of clear spots consisting of nearly colourless matter,
similar to that which composes the spherules. Between the sphe-
rules and the matrix, forming a sharp. boundary, is a clear, narrow,
colourless border (fig. 1, Pl. XXI.), while the matrix itself is tra-
versed by more or less sharply defined lines, which also appear clear
and colourless. |
These lines seem, in places, to be nearly straight, and to divide
* Extract from letter from G. G. Butler, Esq. :—
“With regard to the fragment of spherulitic felstone, I have only to say that
I knocked it off the corner a piece of ‘rock, perhaps 6 or 8 feet square and
2 or 3 high, projecting from,a sloping field on the south side of the road from
- Beddgelert to Capel Curig—about a quarter of a mile from the former place, and
perhaps 200 yards from the road, the field sloping down towards the road.
The rock appeared to be zz situ. I found similar specimens on other protruding
- rocks near, but none so perfect as this. I fear I cannot give any more informa-
tion about it.
* A rock which abuts on the north side of the road, nearly opposite, but not .
so far from Beddgelert (in fact, just at the edge of the village), presents a curious
appearance from a number of globular bodies contained in it averaging 2 or 3
inches in diameter and standing half out from its surface. When knocked in a
careful way, they come out bodily, leaving an empty hemispherical socket.
“T remain, very truly yours,
“G. G. Buruzr.”
404 F, RUTLEY ON THE MICROSCOPIC STRUCTUKE OF
the rock into small irregular cuboidal masses. They also describe
irregular circles or ellipses, the sections of spheres and ellipsoids,
which appear nearly to fill the spaces enclosed by the rectilinear
divisions.
These straight and curved streaks have a very perceptible breadth
(as shown in fig. 5, Pl. XXI., magnified about 12 diameters). Be-
tween crossed Nicols they break up into an infinity of small doubly-
refracting granules; and we may infer that they represent small
fissures which have subsequently been filled by infiltration.
The curved lines seem to indicate a coarse kind of perlitic or
spheroidal structure; and their relation to the straight lines at once
calls to mind the similar phenomena, on a larger scale, in the basalts
of Le Puy and Rowley Regis, described by Pnokesscr Bonney *.
In ane part of the matrix there i is a roundish patch, somewhat less
than 54, inch in diameter, in which evident traces of perlitic struc-
ture are discernible. A portion of this patch, magnified 25 diameters,
is shown in fig. 4, Pl. XXI.
The spherules and spherulitic bands are destitute of any definite
internal arrangement. There is no trace either of radiating or of
concentric structure. Under an amplification of 575 diameters the
spherules are seen to consist of a confused aggregate of extremely
minute, colourless, rounded granules and pale green scales: the
latter appear to be chlorite. The little colourless granules closely
resemble in appearance and in dimensions the granules of spes-
sartine which occur in the Belgian honestones, and which have been
determined and described by Renardt. Owing to their extremely
small dimensions, they fail to occupy the entire thickness of the
section ; hence they are always overlain or underlain by doubly-
refracting matter, which precludes the possibility of ascertaining
whether they are isotropic. On examining a section of the coticule
of Dressante, near Hebronval, in Belgium, given me by Prof. Renard,
I find just the same difficulty, except upon the extreme margin of
the section, where a few of the granules have parted from the pre-
paration, and can be examined independently. In such cases the
light, of course, undergoes extinction during a complete revolution
between crossed Nicols. |
Leturning to the Beddgelert section, a few of the minute colourless
eranules may also be met with in an isolated condition; and their
isotropic character can then be readily recognized. Under these
circumstances we may, perhaps, be justified in regarding them as
garnets, and possibly the manganese garnet spessartiney. There is,
indeed, a honestone, well known to the natives, and occurring in a
quarry at Pen-y-Gwryd at the head of the Llanberis Pass, which,
like its Belgian representative, contains numerous minute garnets
* “On Columnar, Fissile, and Ppheroidal Structure,” Quart. Journ. Geol.
Soe. vol. xxx1i. p. 140.
t Mémoire sur la structure et la composition minéralogique du Coticule :
Brussels, 1877.
i Blowpipe examination of the finely powdered rock shows distinctly the
presence of manganese.
DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 405
identical in appearance with the little grains in the Beddgelert
rock.
From the general character of this rock, from its spherules and
spherulitic bands, and from the vestiges of perlitic structure which
it presents, [ have no hesitation in regarding it as a devitrified obsi-
dian or pitchstone. This might, however, be inferred by any practised
geologist without recourse to the microscope ; and it is only right to
add that Mr. Butler was well aware of its nature when he gave me
the specimen.
The rock next to be described is associated with Bala beds, and
occurs at Clogwyn d’ur Arddu, a high ridge about 1 mile N.W. of
the summit of Snowdon. The specimen from which the section has
been cut was collected long ago by Professor Ramsay*, and is now
in the rock-collection in Jermyn Street.
The specimen is of a greenish grey colour, and shows an interest-
ing weathered surface with projecting bands lying closely together,
and separated by rather deep and narrow furrows. Speaking of
these bands, Prof. Ramsay states that they “‘ probably originated in
the same cause that produced the lamination in the lava of Ascension’’}.
Under the microscope (fig. 2, Pl. X XI.) the section exhibits an irre-
gular wavy-banded structure, such as might have been inferred from
the banded character of the weathered surface. In polarized light this
banding is marked by a strong difference in texture or grain; for the
rock throughout is microcrystalline and is now felstone.
A comparison of this rock with unaltered banded obsidians of com-
paratively late geological age, such as those of Ascension, the Liparis,
the Yellowstone, and other volcanic districts, leaves but little doubt
that the structure has resulted from fluxion; and I think we may
also assume that the rock was once vitreous.
On the right-hand side of the road, between Pont-y-Gromlech
and Gorphwysfa, as we ascend the Llanberis Pass, an outcrop of
dark grey felstone-like rock occurs, which breaks or splinters under
the hammer into irregular slabs or platy fragments. The fissile
structure appears at first sight to be due to the presence of dark
sreenish-black films with an oily lustre, resembling patches of
talecose slate. It is, however, possible that other and more minute
structure may also have some share in imparting this schistose cha-
racter to the rock. In its present condition it may be termed a
felsite schist ; and it is probable that many geologists would, from
the general appearance of hand-specimens, regard it as an indurated
voleanic ash. For a long time the microscopic character of this
rock has been a source of perplexity to me. Under the microscope,
by ordinary transmitted light, the section is seen to be made up of
small fragments, strings, and shreds of every shape, separated by
finely granular and less translucent matter, which is strongly im-
pregnated with avery pale greenish chloritic substance forming very
. * By permission of Prof. Ramsay this description is now laid before the
ociety.
T Descriptive Catalogue of Rock-specimens in the Museum of Practical Geo-
logy, 3rd edit. (1862), p. 42, spec. 874, wall-case 41.
ee. G.S. No..147. 2E
406 ¥F. RUTLEY ON THE MICROSCOPIC STRUCTURE OF
fine strings or films. Fig. 1 conveys a very fair idea of the general
appearance of the section as seen by ordinary transmitted light, and
magnified 55 diameters. Between crossed Nicols the shreds and
Fig, 1.—issile Schist from near Pont-y-Gromlech.
(Magnified 55 diam.)
ZW
RL J
oe Yj
\\
films are shown to be crystalline granular aggregates, which are in
great part quartzose. Under a power giving about 250 diameters,
the matter lying between the shreds appears to consist chiefly of
very minute doubly-refracting granules; and I think that the whole
rock simply presents different textural conditions of felstone, im-
pregnated with some mineral of a chloritic or serpentinous character,
possibly antigorite, since a porphyritic and schistose roek occurring
just above Llyn Teyrn contains better-developed films of a similar
character which closely resemble antigorite. The principal point of
interest, however, is the meaning of the confused assemblage of
many-shaped shreds which impart a distinctive character to thin
sections of this rock. I think that a microscopic examination of
the rhyolite from Gardiner’s River, in Montana, U.S., described and
figured in the paper on the rocks of that country which has already
been laid before the Society, will suffice to show that it is approxi-
mately the same as the rock now under discussion.
I do not believe that the structural peculiarities by means of
which the osteologist correlates the bones of one animal with those
of another, are more trustworthy than the structural peculiarity
visible in these two rocks. A thin section of a deep-red obsidian
from l'olesva in Hungary, given me by Professor Judd, is placed on
the table for comparison with these rocks., When magnified (fig. 2), the
pale glass which constitutes the ground-mass of the section is seen
to be filled with minute strings of a reddish-brown glass, twisted in
the most irregular manner. It will also be seen that the planes of
DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 407
Fig. 2.—Deep-red Obsidian from Tolesva, near Tokay, Hungary.
(Magnified 250 diam.)
section cut off parts of these convoluted strings, leaving irregular-
shaped shreds similar to those in the rocks from Gardiner’s River
and Pont-y-Gromlech, only very much smaller. The shreds in the
latter rock appear, therefore, to be parts of convoluted strings or
bands.
We are thus comparing the Pont-y-Gromlech rock with a distinctly
vitreous rock (obsidian of Tolcsva), on the one hand, and with a rock
which does not present a glassy aspect (rhyolite of Gardiner’s River),
on the other. A question of great interest now arises. Was the
rhyolite of Gardiner’s River once vitreous like the obsidian of Tolesva?
If so, then the Pont-y-Gromlech rock may be a devitrified obsidian.
On the other hand we may be justified in assuming that the micro-
crystalline condition of the rhyolite from Gardiner’s River, and, in-
deed, that of any rhyolite, may be an wnmediate result of cooling, yet
identical with the condition which often supervenes when solidified
glassy rocks undergo devitrification.
We may therefore, | think, be allowed to consider the Pont-y-
Gromlech rock either arhyolite or a devitrified obsidian ; for, in the
first case, it may be regarded as an obsidian devitrified at its birth ;
in the second, as an obsidian devitrified in its oldage. The peculiar
structure of this rock cannot, however, be reconciled with any pro-
cess of crystallization, but must rather be regarded as the result of
fluxion in what, at the time, must have been a nearly or quite
amorphous magma.
These considerations lead me to the conclusion that it is unwise
either to employ too many names for rocks of the same character,
or to give distinctly different names to rocks of different character
which may once have been identical. Still there are difficulties in
framing a new nomenclature; for, if we decline to speak of what
we believe to be a devitrified obsidian as a rhyolite or a felstone, we
2E 2
408 F, RUTLEY ON THE MICROSCOPIC STRUCTURE OF
commit ourselves to opinions concerning former lithological condi-
tions, of which we sometimes have only very imperfect evidence.
Moreover, if we decline to distinguish a rhyolite from an obsidian,
we may with equal justice refuse to recognize a trachyte. It appears
desirable to follow the classification of some of the continental petro-
logists in grouping all the highly-silicated vitreous rocks together
under the term “hyaline rhyolite;”’ and, as our knowledge of this
group increases, we may possibly find that its members differ more
in structure than in any other respect, and that even many of the
structures are common.
I have already stated that the Pont-y-Gromlech rock is now, to
all intents and purposes, a felsite-schist * or felstone. Wherein lies
the difference between a felstone and a rhyolite, so far as mineral
constitution is concerned? The constituents are essentially felspar
and quartz (similar to that in plutonic rocks), the felspar in felstones
being chiefly orthoclase, and that in rhyolites the variety sanidine,
which occurs only in volcanic rocks. In the majority of cases it is
difficult to ascertain with certainty the precise nature of the minute
crystalline granules of felspar in the ground-mass either of a fel-
stone or of a rhyolite. The rhyolites commonly contain more or less
vitreous matter; but in the older examples this, if it existed, has
since undergone devitrification ; and the product is a microcrystalline
ageregate which cannot be distinguished from the rest of the rock,
except perhaps in some instances by difference in texture. The
difference therefore between a rhyolite and a felstone is mineralogi-
cally a very small one. The quartz-rhyolites or liparites are closely
related to quartz-porphyry ; so that here, again, we have a mineralo-
gical affinity in rocks which are, on the one hand, volcanic, and, on
the other, plutonic; and in many cases, :especially among the older
rocks, it is by structure alone that they can be distinguished. The
quartz-porphyries may be regarded as spurs or dykes emanating
from granitic masses ; these dykes, like the margins of the granitic
masses, are commonly poor in mica; or that mineral may be totally
absent. The dykes, again, like the margins of the granitic masses,
‘re usually fine-grained. We have, then, a ae well-defined
series, consisting of :—
dues : Hyaline rhyolites (obsidian, pitchstone, perlite
Eafe Sea sloet | &e.), quartz-rhyolite, and trachyte.
Granitic series ... Quartz-porphyry, and granite. »
Trachyte bears much the same structural relation to quartz-rhyolite
that granite does to quartz-porphyry. Bathymetrical conditions pre-
clude the granitic series from having any vitreous representatives.
That there is a passage from the granitic to the rhyolitic series, as
suggested by many petrologists, seems more than probable. So far
* Tt is here worthy of remark that Daubrée has succeeded in superinducing
schistose as well as fibrous and spherulitic structures in glass tubing, by heat-
ing it in presence of water up to a temperature of about 400° C., and under a
pressure which he estimates at more than 1000 aOR (Etudes Synthé-
tiaues de Géologie Expérimentale, p. 156 eé7 seq.). .
DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 409
as I can judge from microscopic examination of the eruptive rocks
of the Llanberis Pass, the work which remains to be done 1s to fill
in in detail, on a larger scale, the lines now laid down upon the
1-inch map.
I have already laid before this Society a description of a perlitic
rock which occurs at the top of the Glyder Fawr; and I then ex-
pressed my belief that many more devitrified rocks would yet be
found among the felstones of paleeozoic age.
The present paper is probably a very small contribution to this
list; and it is to be hoped that, as the list increases, we shall learn
more precisely what a felstone is, and realize more fully what many
of the felstones once were. The vitreous lavas were probably closely
allied to trachytes. Other eruptive rocks, also occurring in the
Snowdon area, such as those of Llyn-cwm-y-ffynon and Pont-y-
Gromlech, are of a decidedly basic character. Thus we see that, as
it 1s now, so it was in the vastly remote period which we call Silu-
rian. The eruptive rocks of that age were both basic and acid; and
their constituent minerals and structural features were similar to,
if not identical with, those which exist in, but do not specially cha-
racterize the rocks erupted at the present day.
In view of these facts I think we may disclaim any power to
determine the age of a rock by its mineral constitution or structure,
and may protest, as Mr. Allport has done*, against the employment
of different names for similar or once similar rocks, which differ only
in point of age.
APPENDIX.
On the Eruptive Rocks of Skomer Island f.
Since the preceding paper was written I have examined some
specimens from Skomer Island, off the coast of Pembrokeshire. For
many years they have remained undescribed in the collection of
rocks in the Museum of Practical Geology; and my suspicion of their
true nature was first aroused by the close resemblance which one or
two of them bore to other devitrified lavas which I had previously
examined. Microscopic examination of these specimens shows con-
clusively that they are lavas of a once vitreous character. The sedi-
mentary rocks with which they are associated are regarded as
belonging to the Llandeilo or to the Bala series.
Only a short account of the microscopic characters of these lavas
is here given, as they will be examined and described in greater
detail in the forthcoming edition of the official catalogue of the rock-
collection in Jermyn Street.
The specimens about to be described consist chiefly of banded and
spherulitic rocks, now felstones, but once obsidians, the change being
_* “On the Microscopic Structure and Composition of British Carboniferous
Dolerites,” Quart. Journ. Geol. Soe. vol. xxx. p. 565.
+ The following particulars are now laid before the Society by permission
of Prof. Ramsay, by whom also the specimens were collected.
410 F. RUTLEY ON THE MICROSCOPIC STRUCTURE OF
due to the usual process of devitrification; while in some instances
it 18 probable that the rocks have developed a spherulitic structure
throughout, during solidification, in which cases they must be re-
garded as having been spherulite rocks from the first. Although
none of these rocks retain a vitreous appearance, the minute struc-
tures which are developed in them are perfectly preserved, and are
as clearly demonstrable as they would be in the most recent
lavas.
The close resemblance in minute structure between these Skomer-
Island lavas and those of the Yellowstone district in the United
States is very striking, although their respective periods of eruption
are so far removed from one another, namely—by all the time which
elapsed between the deposition of the upper beds of the Lower Silu-
rian series and certainly the lowest, if not the highest, beds of the
Tertiary epoch. There is also a close resemblance between the
Skomer-Island lavas and those of the Snowdon district. The period
of eruption in both areas is nearly the same.
In vol. 1. of the ‘Memoirs of the Geological Survey of England
and Wales’ an account of the rocks of Marloes Bay and Musclewick
Bay is given by Sir Henry De la Beche; but, although Skomer Island
is situated close by, he makes no mention of it. At Wooltack Park,
on the north of Marloes Bay, there are fossiliferous shales with some
sandstones, beneath which it is stated that trap occurs resting on
conglomerate and associated with shales. The whole of the igneous
rocks of Skomer Island and the adjacent promontory have been
mapped as greenstone.
It is, however, evident that Sir Henry De la Beche generalized to
some extent in the mapping of these rocks, as the following extract
from the ‘Transactions of the Geological Society ’* will prove :—
‘¢ All the north of Skomer Island consists of massive trap, having
the character principally of fine-grained compact greenstone, and
sometimes approaching to cornean. ‘The smail peninsula, however,
to the east of the landing-place must be excepted, where some strati-
fied rocks of ambiguous appearance occur. The southern part of the
island consists of stratified greenstone dipping at about 48° to the
south-east. Between this and the greenstone belonging to the north
of the island a quartzose cornean, mostly striped, occurs. In some
parts of the island hornblende is the prevailing ingredient of the
rock.”
In the same paper (at p..2) Sir Henry states that he considers
these traps to be ‘forcibly intruded amongst the other rocks at a
period subsequent to their consolidation;” and he adds that, in
applying the term “stratified” to trap, he only means to imply
‘“‘ that there is a parallelism of texture in the trap, which it has in
common with a contiguous rock belonging to some other formation,
and that this texture is also parallel to the common surface of sepa-
ration between the trap and that other rock.”
* Second series, vol. ii. p. 8.
DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 411
Whether the banded cbsidians, now felstones, are the “ stratified
rocks of ambiguous appearance” is a point which ean only be de-
cided by these who know the ground; or perhaps they may be the
“striped quartzose cornean”’ alluded to as occurring between the
northern and seuthern masses of greenstone which constitute the
island. At all events, Sir Henry’s description clearly shows that
he had not overlooked these rocks, although he does not appear to
have regarded them as lavas, or to have considered them of sufficient
importaice to indicate their position on the Survey map.
Rocks from Skomer Island.
1. Devitrified, banded obsidian.
A compact greenish-grey felstone, petrosilex or hornstone.
Under the microscope the banded structure is very clearly shown ;
and a minute spherulitic structure also occurs in places. ‘The gene-
ral condition of the rock is microcrystalline. A greenish substance
is present in it, which appears to be chlorite. This rock is of much
the same character as the devitrified obsidian or rhyolite from Clo-
gwyn dur Arddu at the base of Snowdon.
2. Devitrified, banded and spherulitic obsidian.
A light greenish-grey to dark blackish-green rock.
The specimen shows a weathered surface, upon which numerous
fine bands stand out in relief. The bands are much contorted.
‘Under the microscope the banding is well shown, and the sphe-
rules are well defined and very numerous. A perlitic structure is
also clearly seen ; and greenish matter in many cases pervades certain
portions of the section. This green matter has in some cases a finely
granular structure, or else contains fine dust, and exercises a weak
depolarization when rotated between crossed Nicols. Spherules of
much larger size than those which constitute the bands are likewise
developed. They interrupt and appear to obliterate the fine sphe-
rulitic bands, which seem abruptly cut off by them. The crystal-
lization in these larger spherules is much more confused than that in
their smaller representatives ; and consequently they show no dark
cross between crossed Nicols.
The structures in this rock are as perfect as any to be met with
in recent lavas.
3. Basalt or andesite.
An iron-grey rock with brown stains, compact in texture and.
showing some minute glistening felspar-crystals.
Under the microscope the rock is seen to be a finely crystalline
admixture of triclinic felspar prisms, granules of augite, and crystals
and grains of magnetite. Some isotropic matter seems also to occur
in the matrix.
4, Quartz-oligoclase trachyte (?).
A greyish rock, with small white porphyritic crystals.
Under the microscope it is seen to consist of crystals of quartz
412 F. RUTLEY ON THE MICROSCOPIC STRUCTURE OF
and triclinic felspars (oligoclase) and orthoclastic felspar, with some
magnetite in a fine microcrystalline matrix *.
The rock No. 4 is possibly the crystalline representative of the
devitrified obsidians. The basalt (No. 3) is evidently an example of
the greenstone which occurs so extensively at this spot. Some of
the obsidians contain large spherical bodies sometimes an inch or
more in diameter, which are best shown upon weathered surfaces.
As these spherules are traversed by the fine bands which pass
through the rocks in which they occur, it seems reasonable to assume
that they have been developed subsequently to the solidification of
the rock.
DESCRIPTION OF PLATE XXI.
Fig. 1. Devitrified spherulitic rock from Beddgelert, showing general character
of spherules and matrix. X18.
2. Devitrified obsidian or rhyolite from Clogwyn d’ur Arddu, Snowdon,
showing banded fluxion-structure. x18.
3. Devitrified spherulitic rock, No. 1. Beddgelert, showing spherules and
spherulitic bands. x6.
4, Ditto, showing portion of a perlitic patch. X25.
5. Ditto, showing parts of spherules at top and right side of field, and
infiltered shrinkage-cracks in matrix. X12.
DIscussIon.
The Cuarrman spoke of the value of the papers ‘and the interest
of the agreement between rocks separated so widely in time or space.
Some of those described by the author might be paralleled by
instances from Arran and from the Auvergne.
Dr. Sorsy said the most interesting part of the paper was the
close relation of the structures described on the one hand to those of
granite, and, on the other, to those of slags. The relation in struc-
ture between slags and the older rocks was of great interest.
Prof. Bonney expressed his sense of the value of the paper. In
his opinion the only difference that could be maintained between
rhyolite and felsite (he thought felstone should be used only as a
group term) was structure; he would understand by rhyolite a
trachytic rock in which a glassy base remained—by felsite those
in which the matrix was crypto- or microcrystallme. He knew
some of the rocks described by the author, and some remarkable
spherulitic rocks, one showing a structure just like that of Pont-y-
Gromlech on the east side of the Glyder.
Rev. J. F. Braxe asked about the formation of the crystals with
an inward growth, and whether large crystals did not indicate slow
cooling.
Mr. BaverMman considered that the irregular strains in the obsi-
dian fragment described by the author might be due to contraction
* The section cut from this specimen was hastily examined on the day upon
which this paper was read ; and I am not sure than it is not a clastic rock.
DEVITRIFIED ROCKS FROM BEDDGELERT AND SNOWDON. 413
consequent on the passage of a glassy into a crystalline substance of
sensibly the same composition ; and instanced the inverse case of the
fusion of felspar, where the increase of volume, in passing to a glass,
fissures the crystal, in the direction of its principal cleavage, into
laminge, which are kept together by the glassy cement.
The AvrHor said that the Arran rocks, so far as he knew, were
intrusive; he quite agreed it would be well to use the term felstone
in a wide sense. Mr. Blake’s question had been answered by Mr.
Bauerman, whose remarks on the fused felspar were of much im-
portance.
414 J. W. DAVIS ON THE FISH-REMAINS OF
32. Nores on the Fisu-remarns of the Bonz-Bep at Aust, near
Briston ; with the Descriprion of some Nuw GunERA and
Species. By Jamus W. Davis, Hsq., F.G.S. &c., Hon. Secretary
of the Yorkshire Geological Society. (Read May 11, 1881.)
[Puate XXII]
I am indebted for the material on which the following paper is.
based to Mr. W. T. Ord, of Bristol, to the Council of the Geolo-
gical Society at London, who have kindly placed their collection at
my disposal, and to Mr. Sollas, Professor of Geology at the
University College, Bristol.
The specimens are in good preservation, the smaller ones, con-
sisting principally of teeth, being unbroken; the larger bones, as
for example, ribs or other bones of Saurians, the larger spines of
Fishes, &c., are generally found in a more or less fragmentary and
broken condition.
From the occurrence of the teeth which are characteristic of the
older Carboniferous rocks, such as Psammodus porosus, Helodus,
and Psephodus magnus of the Mountain Limestone, and Cteno-
ptychius, which has hitherto been found in the Carboniferous
series, and more especially in the Coal-measures, it appears pro-
bable that some of the fossil remains found in the Rheetic beds at
Aust have been derived from the disintegration of the older rocks.
Hither this must have been the case, or the genera of fishes named
had a considerably. longer period of existence than has hitherto
been supposed. It may be objected that the remains are in a very
perfect state of preservation (as, indeed, they are in most cases) and
do not appear to have been exposed to much attrition by being
washed on the shore or bed of the sea or a lake. Itis probable,
however, that the area over which the bone-bed was deposited was
composed, in the neighbourhood of Aust at any rate, of the blue
clays which at present underlie it. During the formation of the
bone-bed the nodular masses of blue-grey stone which are now
found composing a great proportion of its mass were pieces of
clay, rolled round by the action of the waves or tides, so soft that
they received easily an impression of the bones or teeth which lay
scattered along the shore with them. From the immense number
of fossil remains of Saurians and Fish which occur in the bed, it will
be inferred that it required a long period of time for their accumu-
lation, and that throughout all that time there was a peculiar absence
of sedimentary deposits, the nodular masses being derived from the
adjoining Keuper beds, which also formed the floor on which the
bone-bed was deposited.
In a paper read to this Society in 1841* Mr. Strickland showed
the bone-bed to extend over a surface of 120 miles; and since that
* Proc. Geol. Soe. vol. iii. part ii. p. 585. —
THE BONE-BED AT AUST, NEAR BRISTOL. 415
time Mr. Charles Moore, in an elaborate series of papers*, has
proved with extreme minuteness and care that there extended over
the Somersetshire and South Wales Coal-fields, and over the
Mountain Limestone, beds containing Rhetic fossils, the crevices,
veins, and pot-holesin the Mountain Limestone being filled up with
organic reliquiz of vertebrates as well as invertebrates of Rheetic age.
These, according to Mr. Moore, have been washed in during the Rheetic
and subsequent Liassic periods. Such being the case, the circumstances
attending their deposition warrant the supposition that some of the
fossils included in the Rheetic deposits were derived from the
disintegration of the rocks on which they now rest. The bone-bed is
variable in thickness, but rarely exceeds a few inches ; at Aust it is
from 3 in. or 4 in. to 9 in. thick; in many other places it is less,
ranging over considerable areas with a thickness not exceeding one
inch. There is also much diversity in the prevalence of organic
remains. In a few localities the fish-remains occur in abundance,
as at Aust, Axmouth, Coomb Hill, &c., whilst in other places they
are entirely absent or are found very sparingly.
The fishes found in the bone-bed are comprised in the orders
Plagiostomi and Ganoidei, the latter including, according to
Prof. Miall t, the Ceratodus-remains. Besides Ceratodus, the Ganoids
include the genera Saurichthys, Gyrolepis, Lepidotus, and Ambly-
pterus.
Amongst the Plagiostomous genera may be enumerated Hybodus,
Acrodus, Sargodon (?), Nemacanthus, Sphenonchus, Lophodus, Squalo-
raid.
There are also large numbers of bones, teeth, and other remains
of Saurians, including Ichthyosaurus, Nothosaurus, Scelidosaurus,
and others found and identified by Mr. Moore ¢.
A consideration of the characteristics of this mixed group of
organic remains may afford some reasonable basis for deductions as
to the circumstances under which they were accumulated. The
Saurians would undoubtedly exist near and partly on land. The
Ceratodonts, judging from a comparison of the ferms of their teeth
with the still existing Ceratodus of Australia, were vegetable
feeders, and would require a shallow-water area from which to
obtain their food. With respect to the remaining Ganoids, it is
probable that they could freely exist in deeper water, and, from
the character of their teeth, were probably predaceous in their
habits. The Plagiostomous Sharks, with their sharp teeth and
strong fin-spines, often attaining a large size, as evidenced
by the great length of the latter, would be equally adapted
for either deep or shallow waters. Taking all the items
together, it would appear that the Rhetic beds were deposited in
a shallow sea not far from the coast; that the Saurians passed a
large proportion of their existence in the water, the remainder on
* Quart. Journ. Geol. Soc. vol. xvi. p. 483 (1860), vol. xxiii. p. 449 (1867),
vol. xxvii. p. 67 (1881).
t Palzontographical Soc., vol. xxxii. (1878).
t Loce. cité.
416 J. W. DAVIS ON THE FISH-REMAINS OF
the land; of the fishes, the Sharks and some of the Ganoids
frequented the shallow waters, probably in search of food. That
they did so inlarge numbers, and spent considerable time there, is
amply proved by the large number of coprolites.
Microscopical sections of the coprolites exhibit abundant evidence
that the food of the Fishes or Saurians to which they owe their
origin consisted of smaller fishes—fragments of bone, teeth, and
other similar objects belonging to smaller or more slightly armed
species of fish being found in larger proportions than any thing else
with structure. :
Hyszopvus avstirnsis, Davis. (Plate XXII. fig. 1.)
In the third volume of the ‘ Poissons Fossiles’ M. Agassiz described
aspine of Hybodus, of which there were several specimens in the
cabinets of Lord Enniskillen and Sir P. Egerton, and in the museums
at Oxford and Bristol; and an example is figured from the latter, which
is about 6 inches in length. ‘The spine is described as being round
(that is, the sides are not so much compressed); and the ribs are
more prominent, with deeper grooves between than in any other
species described. The ribs do not anastomose, but run parallel to
the anterior portion of the spine, and disappear along the posterior
margin. There isa large cavity along the posterior surface; and the
base of the spine is large proportionally to the remainder. The
examples seen by M. Agassiz did not exhibit any traces of den-
ticles sufficiently well preserved to enable him to describe them.
Dr. Buckland and Sir Henry de la Beche knew ‘the spine, and had
previously considered it a variety of their [chthyodorulites dorsetiensis
(= Hybodus reticulatus, Agassiz) found at Lyme Regis. M. Agassiz
further remarks that H. minor is not a small spine when compared
with others he had described; but, at the same time, the spines
found at Aust Cliff are not of large size, and are very different from
the great spines found in the Lias at Lyme Regis. The teeth
accompanying the spines are also different from those found at Lyme
Regis; and altogether the differences are so great as to necessitate
the institution of a new genus.
Since M. Agassiz wrote his great work, many fossil spines of
Hybodus have been found in the Rheetic beds of Aust; and the
collection at the Bristol Museum contains specimens which very |
nearly approach the sizes attained by the fine examples of Hybodus
reticulatus and formosus of the Lias of Dorset. One of the largest
examples would measure, when perfect, 13 inches in length, and
fully aninch and a quarter in greatest diameter. The base pre-
sents the usual fibrous structure ; it has been deeply and strongly
implanted in the flesh. There is a large orifice or groove opening to
the back of the spine at its base, and afterwards continued as an
internal cavity towards the apex. The width of this orifice, from
back to front, is about double that between the sides of the spine.
The line dividing the base from the exposed portion extends with
a convex curve from the anterior to the posterior portion of the
spine, the convexity being towards the base. The anterior and
THE BONE-BED AT AUST, NEAR BRISTOL. 417
lateral surfaces are ornamented with strongly marked ridges of
enamel, which anastomose frequently, and present a somewhat
wavy outline on account of the enamel forming the ridges not
being of uniform thickness, in some places presenting a beaded
appearance. The ribs lie roughly parallel with the anterior surface
of the spine, and run out along the posterior edge, but not in a
very well defined manner. The junction of the ribs with the basal
portion is not so well defined as in WH. reticulatus: in the latter
the ends of the ribs rise above the surface of the base; whilst in
the Aust specimen the ridges blend with the fibrous structure of
the base, and the hollows between the ridges are below the level
of the basal surface. The anterior and lateral portions of the spine
have a circular or, rather, dome-shaped form in section. The
posterior forms a wide base, not flat, but a little produced outwards
towards the centre. The whole of the posterior portion higher
than the open part of the cavity retains the fibrous structure of
the base; and along each side of the median portion extends a row
of blunt, laterally compressed, enamelled denticles; they are about
-2 inch across the base, and rise *l inch from the surface of the
spine. ach denticle is separated from the next by a distance a
little greater than its own diameter.
These spines differ from those of H. reticulatus in several particu-
lars: their form is stronger and more robust ; the lateral surfaces are
rounder, and the base and cavity wider. In comparison with its
width, the spine is shorter, not so gradually pointed, and less curved.
The posterior denticles are not pointed and recurved towards the base,
as they are in 4. reticulatus; nor do its characters agree with
those ascribed by M. Agassiz to H. minor, as already stated ; and it
appears necessary that a specific name to indicate this spine should
be instituted: I suggest that it be Hybodus austiensis.
Hyszopus punoratus, Davis. (Plate XXII. fig. 2.)
An imperfect spine from the bone-bed possesses characters which
remove it from any other species hitherto described. It consists
of the upper portion of a small spine 1 inch in length; the
antero-posterior diameter is ‘2 of an inch at its broadest part;
the transverse diameter is a little less; the spine is slightly
curved, more so on the anterior than the posterior surface, and
tapers gradually to a point. The lateral surfaces are covered with
longitudinal ridges, separated by grooves of about equal diameter,
numbering five on each side. Along the bottom of each groove
there are a number of minute pittings extending in a line
parallel with the groove. ‘Towards the points the ridges become
less prominent and gradually disappear, the apex being quite
smooth and without strie. There is a row of denticles along
each latero-posterior surface ; they are prominent, obtusely pointed,
laterally compressed. The internal prolongation of the pulp-cavity
is comparatively small (less than one third the diameter of the
spine), situated nearer the posterior than the anterior surface, and
conforming in outline with the oval form of the spine.
418 J. W. DAVIS ON THE FISH-REMAINS OF
Besides Hybodus mimor, the only spine of this genus described
by Prof. Agassiz from the Aust bed was H. leviusculus*. The
original which served for the description of the latter was a small
fragment about half an inch in length, in the museum at Bristol.
It is described as having smooth sides, slightly compressed, with an
internal cavity rounder than the external form of the spine. There
are denticles along the posterior border ; and these are long, pointed,
and recurved towards the base.
The spine I have from Aust, the only other small form of
Hybodus which I have seen, differs in every respect, except size,
from H. leviusculus of Agassiz. Its sides are deeply furrowed; the
posterior denticles are short and blunt; and the internal cavity is
much longer than broad in section.
The number of well-defined species of teeth of Hybodus found in
the Rhetic beds of Aust would lead to the inference that there
should be asimilar variety in the fin-defences of the fishes. Under the
most favourable circumstances it is an extremely difficult matter to
correlate the dermal defences, either spines or scutes, of the Sela-
chians with the teeth of the same genus; but in this instance the
difficulties are greatly increased by the rolled and mixed state in
which the specimens are found; and it appears improbable that
remains will be discovered whose relationship will be rendered
certain by the position or circumstances under which they are dis-
covered. ‘The pittings along the grooves suggest the name punctatus
as appropriately designating this spine.
Remarks on the Genus NeMacantuus, Ag.
This genus was formed to embrace two species of fossil spines of
Selachians found in the bone-bed at Aust. The spines are about 5
or 6 inches in length and °7 inch in breadth in the larger species, viz.
N. monilifer, and little more than half that size in the second one,
N. fiufer. The genus is characterized by the spine having its sides
much compressed, and finely striated, with a small posterior cavity
reaching half the length of the spine ; where the cavity terminates on
the posterior surface there commences. on the sides a number of
rounded tubercles: they originate near the anterior surface, extend
obliquely across the spine, and run in parallel lines thence to its
apex, a row extending along the junction of the lateral with the
posterior face having some resemblance to a row of small blunt
tubercles along each side. Along the anterior portion of the spine
there extends a round keel, which is marked off from the body of
the spine by a lateral canal along each side. In the larger species
the lateral keel is of about the same diameter as the tubercles arranged
along the sides. The smaller species, NV. filifer, differs from the
larger, V. monilifer, in the tenuity of its anterior keel, the smallness
of the tubercles on its sides, and also of those extending along the
posterior edges.
* Poissons Fossiles, tome iii. p. 46, tab. 10. figs. 24, 25, 26.
THE BONE-BED AT AUST, NEAR BRISTOL. 419
In the species described by M. Agassiz the spines are as nearly as
possible twice as much in their antero-posterior as in in their trans-
verse diameter. In a specimen from the Bristol Museum (Plate
XXII. fig. 3) the spine from back to front has a diameter of °35 inch ;
and its width across the posterior surface is *3 inch, or very
nearly equal to the antero-posterior diameter; the external pos-
terior groove is shallow; and no denticles or tubercles are present.
There is a very large median keel along the front of the spine. It
is almost round, but rather wider than deep. It is composed of
shining black enamel, and constitutes one fourth of the entire dia-
meter of the spine. ‘The spine is imperfect, the apical portion
missing ; so that itis impossible to say whether the sides were tuber-
culated. It appears to have been less curved than the common
forms, the portion preserved being straight.
A second specimen, more closely resembling WN. filifer, is a flat-sided
spine of the ordinary kind (Plate XXII. fig. 4), finely striated along
each lateral face. ‘The anterior keel is small and threadhke; along
the posterior surface are blunt, widely separated denticles. This
spine is ‘25 inch in diameter, and, when perfect, would probably be
about 2 inches long. The sides of the spine are covered with
longitudinal striz as in the type specimens.
Both the varieties noticed above are from the collection of Mr.Ord,
of Bristol, and were collected from the bone-bed at Aust Cliff.
Nemacantuvs minor, Davis. (Plate XXII. fig. 5.)
Spine imperfect. Length 1:1 inch, diameter 1 inch, when
perfect probably nearly or about 2 inches in length. In section
it is circular. A canal or internal cavity of similar form ascends
the centre of the spine towards the point (the latter broken off in
this specimen). There is no evidence that the cavity was open
along the posterior surface; but it appears to have been terminal.
The spine is'slightly curved in form. Its surface is slightly and
irregularly grooved, and is further ornamented by a number of mi-
nute papille. In the latter respect the spine resembles the genus
Nemacanthus ; but it differs in other essential respects from either of
the two species described by Prof. Agassiz*. It does not exhibit
any trace of having a ridge of any kind along the anterior
surface ; instead of that, itis round and indiscriminately spotted
with papilla or tubercles. The section of the spine is round, and not,
as in the species of Agassiz, oval or triangular. It appears proba-
ble that the spine may belong to the genus Memacanthus; but it is
quite separated specifically. I propose the name JN. minor in allusion
to its small size compared with those previously described.
The specimen figured is in the museum of the Geological Society
and is labelled “from the Fucoid bed, Wainlode Cliff,” and was
presented to the Society by H. E. Strickland, Esq.
* Poissons Fossiles, vol. iii. p. 26, tab. 7. figs. 9 & 10-15.
420 J. W. DAVIS ON THE FISH-REMAINS OF
Patmosaurus? Srrickianpi, Davis. (Plate XXII. fig. 6.)
In the museum of the Geological Society, London, there is a tooth
which I believe to be unique. It is from the Rhetic bone-bed of
Combe-Hill, near Cheltenham, and was presented to the Society
many years ago by Mr. H. E. Strickland.
The base of the tooth is wanting ; the portion remaining is slightly
more than ‘6 of an inch in length. In section (fig. 66) the
front portion is seen to be more compressed than the back. The
lateral extremities of the tooth are slightly produced, and end in a
serrated margin ascending to the crown or apex of the tooth, which
issmooth. The width nearest the part of the base preserved is -35
inch. The surface of the tooth, except along the lateral margin, is
covered with fine longitudinal striations, which finally disappear
before reaching the point.
This tooth has the appearance of having been washed and water-
worn. The broken portion is smooth and polished ; and it is probable
that it may have been derived from an older rock, and redeposited
amongst the remains of the Fishes and Saurians of the Rheetic age.
At a meeting of this Society held December 15th, 1841*, a paper
was read by Mr. H. E. Strickland on the Bristol bone-bed, in which,
along with other fossil remains, he mentions a “ portion of a tooth
with two finely serrated edges, and considered as probably belonging
to a Saurian allied to the genus Palwosaurus ;” there can be little
doubt this is the same specimen. I have taken the hberty of asso-
ciating the tooth with his name.
SpuEeNoncuus (Hyzopvs) ostusus, Davis. (Plate XXII. fig. 7.)
The genus Sphenonchus was originated by M. Agassiz for the de-
signation of certain objects which are regarded as teeth. It appears
probable, as I shall attempt to show, that these opjects were not
teeth, but dermal defences. The specimen I am about to describe is
‘45 inch in length and ‘35 broad at the base: it is perfect, with
the exception of a small fragment which is broken from the right
portion of the base. The object, which appears homogeneous in
structure, contracts rapidly from the base for a distance of about half
its length. At this point its diameter is little more than a third
that of the basal portion; and it remains the same to within a little
of the point, which is slightly wider and thinner than the stem.
The general form is that characteristic of the genus. It is arched
forward, and does not possess any secondary denticles. The upper
portion is nearly cylindrical, with the point flattened out like a
chisel; near the base the form is three-sided; right and left it is
produced so as to form wing-like processes; whilst down the centre
of the anterior curved portion a third process is developed, which is
continued and increases in size to the lowest portion of the base.
The posterior surface, in its basal portion, is slightly hollowed in-
wards (fig. 76), compensating a little for the ridge in front. The
whole of the surface is smooth and covered with shining enamel.
* Proc. Geol. Soc. vol. iii. pt. 11. p. 585.
THE BONE-BED AT AUST, NEAR BRISTOL. 421
Agassiz, in the third volume of the ‘ Poissons Fossiles,’ describes
three species of this genus :—S. hamatus, from the Lias of Lyme
Regis, in the collection of the Karl of Enniskillen; S. elongatus,
found by Dr. Mantell in Tilgate Forest; and S. Martini, Rob., from
the Portland Oolites of Linksfield. These species vary greatly in form
and general appearance; but in each the generic characters are well
developed. ‘The cylindrical cone forming the upper tooth-like
portion is bent over anteriorly, the basal portion spread out in
aliform processes; and a third median ridge or process is developed
from the anterior surface of the base. The specimen I have de-
scribed from Aust shares these peculiarities ; but in detail it appears
sufficiently distinct to form a new species. It is also from a ho-
rizon earlier and lower than any of those mentioned above; and
though it may probably be found necessary to modity the specific
relationship of these objects when more is known of them, at
present evidence is wanting to indicate that they are not distinct
species.
Sphenonchus hamatus, Agass., is remarkable for its extremely
arched form and the pointed termination of the tooth-like part: it is
an inch in length; and its base is widely expanded. S. Martini, Rob.,
is somewhat similar to S. hamatus, but is shorter and less curved.
The third species, S. elongatus, is much larger than either of the
others; the cylindrical portion is expanded at first, contracting nearer
the extremity, and ending in a second expansion, “en sorte que sa
forme ressemble un peu 4 celle d’une bouteille qu’on aurait recour-
bée.” Sphenonchus obtusus differs from S. hamatus in its smaller size,
less expanded base, and in its curvature being at a considerably
smaller angle: its apical termination, wide, flattened and obtusely
rounded, is in marked contrast to the finely pointed end of S. hama-
tus. S. obtusus has altogether a finer and less stumpy form than
that of S. Martini, whilst from S. elongatus it is easily distinguished
by its smaller size and the nearly uniform diameter of the upper
portion.
I suggest the specific name obtwsus to designate this species, in
reference to its wide and expanded apex. The specimens are from
the cabinet of Mr. Ord.
Prof. Agassiz described the genus Sphenonchus as a member of the
family of Hybodontes, associated with Hybodus, Cladodus, and Diplodus.
Since the classical work of Agassiz was completed, Diplodus has been
proved to be the tooth of Plewracanthus, and must consequently be
remoyed from the family of Hybodontes, and considered in con-
nexion with the spine as nearly associated with the recent Rays,
according to Agassiz; or, as I have attempted to show in a former
communication, it may have some affinities with the group of the
Siluroids. Sphenonchus and Diplodus are referred to in the ‘ Pois-
sons Fossiles’ as offering considerable difference in microscopical
structure from Hybodus and Cladodus, especially the former, which,
whilst having a dense coating of dentine, has a large internal pulp-
cavity, which is very different from the tooth-structure of either
Q.J.G.8. No. 147. 2F
499 , J. W. DAVIS ON THE FISH-REMAINS OF
of the others. In the Magazine of Natural History* Mr. Charles-
worth has described the fossil remains of a species of Hybodus, col-
lected by Miss Anning at Lyme Regis. In connexion with the
spine and teeth there is a bone which is undoubtedly an example of
Sphenonchus, and is regarded by Prof. Agassiz in that light; im the
same volume (p. 605) there is a letter from Miss Anning, saying .
that the hooked tooth (Sphenonchus) is by no means new, but that it
has been frequently found at Lyme Regis in connexion with the
teeth and spines of Hybodus or the teeth of Acrodus.
Mr. Charlesworth suggested that the hooked tosth is a dermal
appendage or defence, probably situated immediately behind the
head. Specimens since discovered prove that this suggestion was
correct, and that two or three of these bodies were located on
the occipital region of the head of Hybodus. The microscopical
structure of the teeth and dermal defences of the Klasmobranch
fishes is very similar, one of the principal differences being the
large size of the pulp-cavity of the dermal processes as compared
with that of the teeth ; and in this respect Prof. Agassiz has shown
that there is a great difference between the teeth of Hybodus or
Cladodus and Sphenonchus. The base of Sphenonchus is excessively
expanded, especially in S. hamatus from the Lias; and its fibrous
structure without enamel indicates that it was imbedded in the
flesh ; it appears in this respect to resemble the dermal defences of
Raia clavata from the Tertiary deposits.
In addition to the specimens already named, there are a number
of the bones of the head, including jaws with teeth, of Saurachthys ?;
these I have handed to Mr. Sollas, who has already in preparation a
paper on the same genus, derived from the examination of similar
Specimens in his possession.
Large numbers of fragmentary bones and small teeth are found
scattered throughout the mass of the bed, but without sufficiently
well established characters to enable an account to be given of them.
A large operculum, nearly 24 inches in diameter, probably belong-
ing to Ceratodus, and several bones with articular extremities,
which may belong to the same genus, are included in the collection
of Mr. Ord.
Besides the palatal teeth of Psammodus and Cochliodus, in all
probability derived from the Mountain Limestone which underlies
the Rhetic beds in some parts of the area, the following species of
Ctenoptychius have probably been derived from the Coal-measures,
and the Petalodus from within the Coal-measures or the Limestone.
Specimens of Helodus have also been met with; they appear to be-
long or are very nearly related to H. semplew.
Crenoptycuivs Orpi1, Davis. (Plate XXII. fig. 8.)
Tooth. Length -55 inch. Depth -3inch. A portion of the base
is wanting.
The superior surface is folded so as to form a pectinated edge
* Vol. ili. p. 242, 1839.
THE BONE-BED AT AUST, NEAR BRISTOL. 493
extending along the crown, which occupies the greatest diameter of
the tooth. It is slightly circular towards each end, the central
part being almost straight. It is very thin, and appears to have
constituted a sharp cutting-edge. The foldings are produced at their
extremities into small and separated denticles, about 24 in number,
whose diameter is greater from back to front than laterally. Some
of these are broken at the tips; and the section thus exposed, when
magnified, shows that a hollow tube ascended in the centre of each.
The sulci descending to the body of the tooth from the denticula-
tions are much more marked towards the lateral extremities than in
the median region. Towards the base the tooth becomes gradually
thicker ; at the same time it also converges laterally to two thirds the
diameter of the crown; from this part the tooth is broken off; but,
from the impression on the matrix, it appears to have terminated in
a broadly expanded rounded base. The tooth is attached to the
matrix; and consequently the posterior surface is not exposed. The
whole of the upper part of the anterior surface, above the root or
base, 1s covered with a smooth polished surface of ganoine. From the
base of the plications or foldings forming the crown of the tooth the
surface extends towards the base in the form of a semicircular
hollow.
This genus of Selachians was instituted by Agassiz (Poiss. Foss.
tom. 1. p. 99) for the accommodation of teeth obtained from the
Coal-measures of Staffordshire and Lancashire. Since that time
specimens have been found in the Limestone of Armagh, and also
in the Coal-measures:and Limestones of Virginia, Illinois, and other
localities in America. Hitherto specimens of the genus have been
restricted to the Carboniferous group of rocks,
The specimen now described may either have been derived from
the disintegration of coal-measure strata, and washed into the
Rhetic beds during their deposition; or it may have belonged to
a fish which lived during the period when those deposits were
accumulating. It is probable that the former is the correct sup-
position.
The species from Aust differs materially from the type species of
Agassiz, C. apicalis. The latter is possessed of only seven or eight
protuberances from the crown of the tooth, the centre one being
considerably larger and forming an apex to those on either side.
C. semicircularis, N. & W., irom the Coal-measure limestone of Ohio,
bears a remarkably close resemblance to C. apicalis of Agassiz,
and seems to be so little removed as scarcely to necessitate a sepa-
rate specific name. Ctenoptychius Ordw bears some resemblance
to C. denticulaius, Agass. (loc. ct. p. 101), in possessing a large
number of serrations closely ranged along the crown of the tooth,
whose lower portions form a series of plications extending to the
body of the tooth and there disappearing; but in C. denticulatus the
curvatures extend quite straight across the crown, whilst in the
Aust specimen they form a semicircle. The base of the tooth in
C. denticulatus is also much wider than in C. Ordii.
Ctenoptychius serratus, Ord (Sedgw. and M‘Coy, Brit. Pal. Fos-
2F 2
424 J. W. DAVIS ON THE FISH-REMAINS OF
sils &c. p. 626, pl. 3. i. figs. 21, 22, 23), from the limestone of
Armagh, bears a greater resemblance to this specimen than, perhaps,
any others; but it may be easily distinguished by the greater
breadth of the crown of the tooth compared with its depth, the com-
paratively wide and short, somewhat cone-shaped character of the
denticles, and the tips of such denticles appearing minutely crenu-
lated under the lens.
The specimens serving for the above descriptions were collected at
Aust by Mr. Ord, and are from his cabinet. In recognition of his
energetic and painstaking labours, I have ventured to employ his
name to distinguish this species of Ctenoptychius.
CrENOPTYCHIUS PECTINATUS, Ag.
A second species of Ctenoptychius has also been found at Aust,
and forms a part of the collection of Mr. Ord, of Bristol. It is -2
inch across the crown, and has a depth from the upper edge of
the crown to the base -15 inch. The crown is composed of
about 12 denticles, the tips of which extend almost in a straight
line; at the apex the denticles terminate in short pointed cones.
Towards the body of the tooth these speedily coalesce and form
plications extending more than half the distance towards the base;
they form a concave surface anteriorly, the base becoming thicker
and convex. The two outermost denticles, stronger than the re-
mainder, are continued in a semicircle, and converge towards the
base. The whole of the exposed surface is covered with a black,
shining enamel.
In the third volume of the ‘ Poissons Fossiles’*, M. Agassiz
describes and figures under the name of Ctenoptychius pectinatus,
some small teeth obtained from the Burdie-House Limestone. The
specimens figured present very considerable variations in form, but are
each characterized by the denticles forming the crown of the tooth
being less distinctly separated towards the apex, and the points,
instead of extending vertically, as in C. apzcalis, diverge or radiate
from the centre, somewhat in theform of a fan. The beautiful little
specimen from Aust agrees sufficiently well with this description to
warrant its inclusion in the same genus and species. Its more
rounded basal termination is the most striking point of divergence,
C. pectinatus haying a more contracted stem-like or prolonged basal
portion.
Crapopus curtus, Davis. (Plate XXII. fig. 9.)
This tooth offers some peculiarities which give it a distinctive
character. Itisimbedded in the matrix ; and on the lower part it is
slightly imperfect. It consists of a wide and thick base, from the
centre of which springs a cone-shaped cusp. On either side the
central cone there are indications that at least one secondary cusp
has existed. The bony structure is very dense, and now of a deep
brown colour. The length of the base is -4 inch; and the
height of the central cone is ‘3 inch. The latter is rather less
* Page 100, tab. 19. figs. 2, 3, 4.
ean
THE BONE-BED AT AUST, NEAR BRISTOL. 425
than °2 inch in diameter, and it ends in a rounded apex; rising
from the body of the tooth, it first curves a little outward and
backward, and then again bends forward, the end projecting, as
shown in fig. 10a, Pl. XXII. It appears to be thin in proportion to
its width, and has quite a tongue-shaped appearance. The surface
of the part of the tooth forming the cone is deeply indented with
numerous pituoles. The tip is smooth and is covered with a thick
coating of ganoine. The basal line of the lower portion of the tooth
is curved inwards from each lateral extremity ; and from the cone
the tooth swells with a well-rounded forward curve to the base.
Near each lateral extremity of the base a part has been broken away
with the matrix. The portion left exhibits the base of a secondary
denticle or cone, in the centre of which is the cavity which as-
cended towards its point. The secondary denticles were placed
forward in comparison with the principal centre one, and were
rounder in section.
This specimen more resembles Agassiz’s species C. marginatus
than any other; it may be easily distinguished, however, by the
absence of the deeply striated surface which characterizes the
latter and by its shorter base. I suggest the nomen triviale C.
curtus.
EXPLANATION OF PLATE XXII. figs. 1-9.
Fig. 1. Hybodus austiensts, Davis.
2. Hybodus punctatus, Davis.
2a. Transverse section.
3. Nemacanthus monilifer, var. a.
3a. Transverse section.
4, Nemacanthus monilifer, var. 3.
4a. Transverse section.
5. Nemacanthus minor, Davis.
5a. Portion of spine, magnified.
5b. Transverse section.
6. Paleosaurus Stricklandi, Davis.
6a. Tooth, magnified.
6. Transverse section, nat. size.
7. Sphenonchus obtusus, Davis.
7a. Ditto, magnified.
76. Antero-lateral form.
7c. Posterior view.
7d. Postero-lateral form.
8. Ctenoptychius Ordit, Davis
8a. Longitudinal section.
9. Cladodus curtus, Davis.
9a. Longitudinal section.
Discusston.
Prof. SreLry remarked on the curious survival in the Aust deposit
of Paleozoic types of fishes mingled with forms peculiar to the
Mesozoic as offering a parallel to the mixture of Paleozoic with
Secondary Mollusca in the Upper Trias of the Austrian Alps. He
426 ON FISH-REMAINS FROM BONE-BED AT AUST, NEAR BRISTOL.
stated that Sphenonchus always occurs on the head of Hybodont
fishes in the Secondary rocks.
Mr. Tawnzy thought the Paleozoic forms in the Aust bed are
fossils derived from the Carboniferous strata, and not, as Prof.
Seeley contended, surviving types.
Mr. Lonek stated that there is a great difference between the
contents of the bone-bed at Garden Cliff at Westbury and Aust Cliff
respectively. He thought the fossils in the bone-bed do not belong
to the period at which the materials were accumulated.
Mr. Ussuer thought that the working-out of the Rhetic beds
might afford evidence of the unconformities due to changed condi-
tions of deposit. He alluded to an appearance of unconformity
between Rheetic and Trias at Newark, where a thin band of derived
fragments occurred at the base of the former.
Rev. H. Wiywoop argued against the theory of the bone-bed
being a remanié bed from the fact of the delicate fossils in it not
pone waterworn.
The Prestpent thought that most of the fossils at Aust Cliff and
Westbury are not remanié, but are of the true Rhetic age; but
some Carboniferous forms are undoubtedly derived. The specimens
of Ceratodus were not at all worn. The form called Sphenonchus
is certainly the head-spine of Hi yoda as proved by specimens
from Lyme Regis.
The ArHoR. stated that the details that he had given represented
the examination of only three collections; and that there yet remained
much work to be done in this field.
Quart Journ. Geol. Soc Vol. XXXVI PLA
Mintern Bros. ump
AS. Foord del etlith
=MAINS FROM THE AUST BONE-BED
FISH BEM NE CDAL-MEASURES
ae)
wh
Sie
,
*
5 : s
ae
;
5
.
.
*
J. W. DAVIS ON ANODONTACANTHUS, 427
33. On ANODONTACANTHUS, @ NEW Gunus of Fosstt Fisnus from the
Coat-MEASURES ; with Descriptions of three New Sprcres. By
James W. Davis, F.G.S. &. (Read May 11, 1881.)
[Pirate XXII, ]
THe spines which form the subjects of the following descriptions
are from the West-Riding Coalfield in Yorkshire, and the Ironstone
occurring in the Lower Limestone series near Edinburgh. A strati-
graphical description of the Cannel Coal at Tingley, from which the
first two species have been obtained, may be consulted in the
Quarterly Journal of the Geological Society issued for February
1880, page 56.
The three species of Ichthyodorulites forming the subject of this
paper are the only specimens of which I have cognizance possessing
their peculiar characteristics. In some particulars they resemble
the genus Pleuracanthus; they are composed of a strong, close-
grained, fibrous substance. ‘Their general form is also similar to
that of the Pleuracanths: the internal cavity is terminal at the basal
extremity ; and the walls become thinner near the base in comparison
with the remainder of the spine; the method of implantation in the
body of the fish must also have been the same. The great distin-
guishing feature between the two rests an the absence in this genus
of any form of denticulation. In the Pleuracanths there are two
rows of denticles either along each lateral surface or on some portion
between the lateral and posterior lines. Whether this may be a
sufficient distinction to necessitate a second genus, or further ‘dis-
coyeries will prove that it must be included in the genus Plewra-
canthus, remains to be seen; but for the present it may be better
to consider it as a distinct genus, for the following reason : hitherto
remains of the fish Plewracanthus, where found in even tolerable
perfection, as in the Stone-coal of Bohemia, have always had associ-
ated together the three-pronged teeth of the so-called Diplodus, and
a spine, the latter more or less straight, but always possessing, in one
situation or another, two rows of denticles. From Tingley, where the
spines under discussion have been obtained, I have several slabs of
Cannel Coal covered with a mass of cartilage full of the mosaic-lke,
minute, rhomboidal, bony centres characteristic of Plewracanthus,
with numbers of teeth, and occasionally a spine in situ; but in all
cases the spine has been denticulated. So far all the evidence goes
to show that the spines of Plewracanthus were armed or ornamented
by these denticular appendages; there is a possibility, however, that
a specimen may be found with a spine without denticles in association
with undoubted Plewracanthus-remains ; and should that happen, it
will be necessary to modify the character of the genus so as embrace
thisone. Until such evidence is forthcoming, it may be regarded as a
distinct genus, for which the name Anodontacanthus may not be in-
appropriate, signifying a toothless spine.
428 J. W. DAVIS ON ANODONTACANTHUS, A NEW GENUS
1. Anopontacantuvs acutus, Davis. (Plate XXII. fig. 10.)
Spine. Length 2°5 inches, breadth :2inch. The spine is straight,
and gradually tapers to a point; there are no denticles; and
the surface of the spine is uniformly covered with little pittings,
giving an appearance of reticulation. The walls are about one
fourth the diameter of the spine in thickness; there is an in-
ternal cavity with a wide open termination at the basal extremity,
the walls as they approach the base becoming much thinner. The
cavity extends along the interior of the spine almost to its apex.
The spine has every appearance of having originally been circular in
form. It has, however, become somewhat crushed along the basal or
weaker portion of the spine since its deposition. The specific desig-
nation acutus expresses its pointed character.
Locality. Cannel Coal, Tingley, Yorkshire.
2, ANODONTACANTHUS oBTUSUS, Davis. (Plate XXII. fig. 11.)
A spine from the same locality and horizon as the one already
described is of larger dimensions and different form ; the basal end
is broken off; the remaining portion is 2°5 inches in length, and the
diameter nearly 0°3 inch. Judging from the proportions of the
spine preserved, it is probable that, including the missing portion,
its length would be 3:50 inches when perfect. The surface is uni-
forinly covered with minute longitudinal striations, which towards
the apex become broken up into small pore-like indentations, the
latter being finer than in the smaller species. The portion of the
spline preserved maintains a uniform thickness to within an inch
of the apex, where it becomes slightly contracted, and ends in a
broad, flattened, obtusely rounded extremity, 0°2 inch across. The
body of the spine is oval in section, with an internal canal occu-
pying one third of its diameter. The spine differs from the one de-
scribed before in its greater size, oval form in section, extremely
broad apical termination, striated surface, and im the greater
thickness and strength of its walls. All together these differences
appear sufficiently great to render necessary a separate specific de-
signation ; and I propose to give it the name of A. obtusus, in refer-
ence to its obtusely-pointed extremity.
Locality. Cannel Coal, Tingley, Yorkshire.
3, ANODONTACANTHUS FasTIGIATUS, Davis. (Plate XXIT. fig. 12.)
Spine imperfect, the base absent; part preserved 2-4 inches in
length, extending from the point, apparently half the length of the
spine, the lateral diameter greatest, being 0-4 inch. It is oval in
section, least diameter between the anterior and posterior faces being
0-2 inch; there is a central cavity, circular in section, which
extends towards the point. From the largest diameter of the spine,
it becomes gradually smaller, and ends in a somewhat worn-looking
point. The whole of the surface is covered with longitudinal strie,
most distinct near the basal extremity, anastomosing and becoming
gradually less numerous towards the point, where the striz have
disappeared and the spine is smooth,
OF FOSSIL FISHES FROM THE COAL-MEASURES. 429
This specimen is evidently closely related to the two species already
described from the Cannel Coal, though it varies somewhat in form.
It is larger and stronger in appearance ; as compared with the others
it is very broad towards the base, and contracts in diameter more
rapidly to the point. Itis oval in section, in this particular resembling
A. obtusus, whilst it differs from A. acutus, which is round ; all the
three agree in being straight, ending in a more or less pointed apex,
and in the absence of denticles. The spines are of the same dense
structure in each ; and the form of the internal cavity appears to be
similar. In reference to its tapering form, I suggest the specific
name fastigiatus.
Locality. Blackband Ironstone at Loanhead, in the Middle Lime-
stone series near Edinburgh. The specimen has been sent to me by
Mr. W. Tait Kinnear of that city.
EXPLANATION OF PLATE XXII. figs. 10-12.
Figs. 10, 10a. Anodontacanthus acutus, Davis.
Fig. 10d. Transverse section.
11. Anodontacanthus obtusus, Davis.
11 a. Transverse section.
12. Anodontacanthus fastigiatus, Davis.
12a. Transverse section.
430 P. B. BRODIE ON CERTAIN QUARTZITE AND SANDSTONE
34. On certain QuartzitE and SanDstonE FossItiFERous PEBBLEs in
the Drirr in WARWICKSHIRE, and their probable Ippntity, litho-
logically and zoologically, with the true Lownr Strur1an PEBBLES
with similar Fosstts im the Trias at BupierenH SALrerton,
DevonsuirE. By the Rev. P. B. Broprn, M.A., F.G.S. (Read
May 11, 1881.)
Specrat interest and some little difficulty attaches to the history
and origin of certain quartzite and other pebbles in the Drift in a
limited portion of the Midland Counties, which it is desirable, if
possible, to determine. With this object I beg leave to lay a few
more additional particulars before the Society, which will form a
supplement to my previous paper in the Quarterly Journal, vol. xxiii.
p- 210, 1867. It seems probable that the Keuper sandstones and
marls in the more central parts of England were at one time much
thicker, before denudation had reduced them, and that the pebble-
beds existed in them as at Budleigh Salterton, and were afterwards
broken up and the pebbles (like the flints of the Chalk) scattered
about in all directions by powerful currents of water, helping to
form a large proportion of the Drift in this and other parts of the
Midlands. In a short notice in the Geological Magazine (July
1878), Mr. 8. G. Percival supposes that the quartzose and many
other pebbles in the Drift of the Midland Counties were originally
derived from the Bunter conglomerate. This may be probable in
some slight degree; and Mr. Jennings, in the Geological Magazine
(May 1878, No. 167), states that he has found Orthis redux (bud-
leighensis) in a supposed Bunter pebble near Nottingham, where a
careful search should be made for other fossils which may occur
there in situ, both in the Conglomerate and the Drift—viz. the
igantic Lingule so characteristic of the lower Silurians in Nor-
mandy, some of which I have already detected in the Drift at
Rowington. If it can be shown that these pebbles in the Drift were
originally derived from the Bunter, the latter must have been
broken up before they were deposited in this newer portion of the
Trias; then comes the question, Whence were these pebbles derived
in the first instance, before they were washed, first into the Bunter
(helping to form the Conglomerate), and afterwards into the later
New Red Sandstone, as they certainly were, in Devonshire and
other places? |
The fossils found in these pebbles here and elsewhere show
that many belonged to Paleozoic rocks, as evidenced by Orthis
budleighensis, Lingula Leseuwru, Trachyderma serrata, and some
others given in the list at the end of this paper. Some of these,
especially the Lingulw, are species which as yet have not been
noticed anywhere wm situ in this country, but are peculiar to Nor-
mandy and Brittany, and were determined by the late Mr. Salter.
Mr. Pengelly (Geol. Mag. No. 167, 1878) thinks that the occurrence
FOSSILIFEROUS PEBBLES IN THE DRIFT IN WARWICKSHIRE. 401
of Orthis budleighensis in the altered quartz rock (Lower Silurian)
of Gorran Haven, Cornwall, shows that some of the Budleigh pebbles
were derived from there, which may be the case so far as regards
the Devonian area, but would hardly account for their presence so
much further to the north-east, in some parts of the Midland Coun-
ties for example.
Therefore I suggested a more northerly or north-easterly exten-
sion of Old Silurian rocks, in which view my late lamented friend
Professor Phillips concurred. This would bring them much nearer
to that portion of England now forming the Midland District; and
the destruction of those ancient palzozoic deposits may have largely
helped to supply the Bunter with pebbles, which were in later times,
by the denudation of the latter, washed into the New Red Sandstone
then forming. This, again, in its turn, was greatly attenuated, and
the pebbles, much reduced in bulk, finally distributed, with many
others derived from rocks of diverse ages and from all parts (north,
south, east and west, notably from the north), as Drift.
With reference to the Bunter Conglomerate on the northern edge
of Cannock Chase, Professor Bonney, in a paper in the Geological
Magazine for September 1880, concludes, from a careful comparison
of the quartzite at Loch Nearn in Scotland, that many of the Staf-
fordshire Bunter pebbles were derived from the north-west of
Scotland. Other and different quartzites, he says, resemble more
closely those of Budleigh, the Lickey, and Hartshill. He found
Orthis budleighensis in a pebble at Rugeley which was identi-
fied by Mr. Etheridge, and was, he states, lithologically and
zoologically identical with the Cornish and Budleigh specimens.
He also noticed a Rhynchonella, and probably Orthis calligramma.
In Mr. Percival’s collection of pebbles from the Drift at Mose-
ley, Birmingham, in the Jermyn-Street Museum, the following
fossils are recorded—Orthoceras?, Cleidophorus amygdalis, Orthis
budleighensis, Stricklandima lyrata, Spirifera disjuncta, Glypto-
erinus, Petraia bina*. Professor Bonney is of opinion that the Lickey
_ largely contributed to the Bunter pebbles about Birmingham and
Bromsgrove. I quite agree with him in thinking that none of the
Midland-Counties pebbles came from South Devon, and with Prof.
Hull that very many have a northern origin; but there many others
in certain places, and notably in the area referred to in this paper,
* Some time since, I looked over a miscellaneous collection of rocks presented
by Messrs Allport and Percival to the Midland Institute, obtained by them from
the Drift in the neighbourhood of Birmingham, chiefly from Moseley and other
places adjacent. There are many igneous and metamorphic rocks, basalt, gra-
nite, syenite, and hard crystalline pebbles, including agates, all of which occur
at Rowington. The fossiliferous rocks are chiefly Carboniferous, including chert
with encrinite stems, probably from Derbyshire, several shells and corals and coal-
plants. There are few (if any) Llandovery species. There are some Orthides,
some of which occur in a dark-grey boulder very like the Snowdon rocks.
There are only a few quartz pebbles similar to those described in this paper ;
but I observed among them Orthis budleighensis and Trachyderma serrata of
large size and well preserved, but certainly, taking the whole collection, not so
numerous as in the Drift in this district.
432 P. B. BRODIE ON CERTAIN QUARTZITE AND SANDSTONE
which must have had a different origin. Very likely the altered
Llandovery Sandstone (quartz rock) of the Lickey contributed many
of the pebbles in this Drift, though it would be almost impos-
sible to determine the source of all the quartz pebbles in the latter;
I have, however, not yet detected a single well-defined Llandovery
species in any of them in this district; and a very considerable num-
ber, if not a majority of the fossils in the pebbles I have obtained are
decidedly of Lower Silurian origin ; so that in a direction south of
Birmingham and towards Warwick and Stratford-on-Avon the
tendency evidently seems to be that pebbles of lower palseozoic age
predominate; and the lithological and zoological resemblance which
they bear to the pebbles of this date at Budleigh is sufficiently close
to lead to the conclusion that they are in all respects identical and
were derived from some Old Silurian rocks at a greater or less dis-
tance, and so far had a common origin. Originally, of course, they
must have come from their parent paleeozoic rock wherever it was,
by the wear and tear of which, by the action of waves and currents
and other processes of denudation, in the course of ages they became
pebbles, and may have been in the first instance, perhaps, washed
into the Bunter and have helped to form a portion, greater or less as
the case might be, of its conglomerates in certain places. When this
was in its turn fractured and denuded, some of these pebbles may
have been afterwards redeposited in the New Red Sandstone, not
everywhere, but locally, as at Budleigh in Devonshire, and parts of
Warwickshire*. When the latter was also largely denuded, these
Old Silurian bouldered remnants were finally scattered about and
mingled with the Drift. If not derived from the Bunter or the New
Red Sandstone they must have come directly from the relics of some
ancient Silurian formation which was still in existence, and was
finally but partially broken up at a more or less distant period,
thus helping to add largely to the widely accumulating, often sifted
and re-formed Drift.
In a redistributed and miscellaneous superficial deposit of pebbles
and other débris, like that of the Midland Counties in the districts
referred to, it would, I think, be incorrect (at least we have not
sufficient evidence as yet) to infer that most of the quartzite and
other pebbles are derived from the Bunter. A large majority of
these are more or less consolidated quartzite; and I have one pebble
of quartz with an obscure impression of a shell, which reminds me
of the Cornish Lower Silurian rock at Caerhayes. The most abun-
dant are grey and brown, more or less striated, consolidated sand-
stone boulders, varying in size and sometimes of a deep red colour;
and these agree lithologically with the Budleigh pebbles containing
* Although, with the exception of the Lower Keuper sandstone at Budleigh,
there are no pebbles elsewhere found in situ in the New Red Sandstone, there
is no reason why they should not have occurred in certain places in other di-
rections in the same formation, either in the Upper or Lower Keuper. In the
Midland Counties the upper division has here and there undergone very ex-
tensive denudation ; or possibly pebble-beds may still exist in the New Red which
have not yet been discovered.
FOSSILIFEROUS PEBBLES IN THE DRIFT IN WARWICKSHIRE. 433
certain well-known Silurian species and some of the rock specimens
I have from Normandy. In fact placing the majority of the War-
wickshire Drift pebbles in my collection side by side with those from
Devonshire and France, it would be impossible to separate them,
the character of the rock being identical, and the fossils, where pre-
sent, the same. This is a point of much interest, and while fossili-
ferous pebbles are on the whole rare (though, of course, very many
must have been overlooked), there are many which have the same
mineralogical character, and really form a considerable portion of
the gravels, and were, no doubt, derived from the same source and
originally belonged to a formation of the same age. With the
exception of a few Carboniferous fossils and others of later date a
very large percentage belong, as it appears, to the older Silurian
rocks, and wherever they may have occurred a situ must have been
originally derived from them. The absence, apparently, of Llan-
dovery fossils is remarkable, and seems to show that a very small
proportion of the Drift in this district had come from the Lickey
within sight and not so very far off. In a list of fossils from
the Bunter conglomerates near Cannock Chase, Mr. W. Molyneux*,
F.G.S., on the authority of the late Mr. Salter, assigns all the species to
Mountain- Limestone and Upper Silurian(May Hill sandstone, Llando-
very) groups, and not one Lower Silurian form occurs; but Professor
Bonney records Orthis redux (budleighensis) + from the same district
on the authority of Mr. Etheridge. Mr. Davidson¢ is of opinion that
the majority of the Brachiopoda in the pebbles at Budleigh are
Devonian, which predominate; but the Lower Silurian are sufficiently
numerous and well preserved to have enabled Mr. Salter || to deter-
mine and identify a considerable number with certain species, giant
Lingule and others, peculiar to the district of May and Gehard,
(Armorican sandstone) in Normandy.
The small collection of Lower-Silurian fossils which I possess, the
result of several years’ work, from a limited area of the Midland
District, must have been derived from a much nearer source than
Devon or Cornwall; and Professor Bonney, in the same paper, justly
observes that, as from physical considerations it is almost impossible
that Cornish pebbles could have made their way into the country
round Cannock Chase, the only possible inference is a nearer one by
a further extension to the north-east of the old Silurian strata with
their fossiliferous sandstones and quartzites. The idea that they
can have been derived directly from Normandy is, of course, out of
the question ; and Mr. Davidson also contends for an extension, as I
do, of Silurian rocks in the Channel and nearer to Devonshire as a
* Proceedings of the Dudley and Midland Geological and Scientific Society,
1877, p. 139..
t Ate A. H. Atkins, B.Sc., one of the masters of King Edward’s School, Bir-
mingham, has lately found Orthis budleighensis, in situ, in one of the Bunter
pebble-beds, at Kinver Edge, near Stourbridge, which is another instance of
the presence of this species in the lower division of the Trias. I recognized
the species at once, and Mr. Davidson has since confirmed it.
¢{ Quart. Journ. Geol. Soe. vol. vi., February, 1870, No. 101.
|| Quart. Journ. Geol. Soe. vol. i1., August, 1864, No. 79.
434 P. B. BRODIE ON CERTAIN QUARTZITE AND SANDSTONE
probable source of the Budleigh pebbles which contain fossils of
that date. The extension of this area of ancient rocks, or, indeed, of
any geological age, is never improbable when we consider the
enormous amount of denudation which all great formations have at
one time or other undergone. I have made some additions to
the Lower-Silurian fossils I have detected in the Warwickshire Drift
since the publication of my former paper on this subject in the
Journal of the Geological Society (vol. xxiii. p. 210, 1867); Orthis
redux and Lingula Lesewrt were determined by Mr. Woodward some
years ago ; Lingula, n. sp., by Mr. Davidson, and the remainder by
Mr. Etheridge, who has been kind enough to examine them; and I
here give the entire number, with the additional species, on his
authority :
Orthis budleighensis. Lyrodesma celata?
Valpyana. Ctenodonta Bertrandi ?
Lingula Leseurii, n. sp., Davidson. Arca Noranjoana ?
Spirifer antiquissimus ? Palearca secunda.
Davidis? Trachyderma serrata,
Rhynchonella sp. Calymene Tristani.
Modiolopsis lirata. Homalonotus, portions.
sp. Fucoids, one or two branching forms.
Orthis budleighensis is very abundant and characteristic. One
of the Lingule determined by Mr. Davidson is, he says, a new
species and totally unlike any of those from Budleigh. The
Annelid Trachyderma serrata is frequent and generally in good
preservation. The total number of Lower-Silurian genera and species
figured and described by Salter from the pebbles at Budleigh Sal-
terton is twenty-four; and there are several diligent collectors of -
these fossils in Devonshire. From the Midland Drift, in a limited
space and with less facilities for obtaining them, I have procured
sixteen, leaving only a difference of eight in favour of Devon—which
is somewhat remarkable, considering the much better opportunities
for collecting them in the West. At present, I believe, this is the
largest number of Lower-Silurian fossils of the age, probably, of the
Bala and Lower Llandeilo formations, hitherto observed in the Mid-
land Drift. This fact too, I think, strengthens my argument in
favour of more extensive ramifications of old paleozoic rocks in a
north or north-easterly direction; and these, when broken up, would
furnish ample materials coming from different areas to supply the
fossiliferous pebbles referred to. No doubt this list would be
largely increased if the road-heaps, collected chiefly from the fields,
could be more diligently searched; for many fossiliferous pebbles
must be overlooked.
Mr. Walter Keeping, in an interesting paper * on the Upware and
Potton Greensand pebble-beds, observes that “some of the quart-
zites are like those of the New Red Sandstone pebble-beds, and were
probably thus derived.” He accounts for the presence of other older
paleeozoic pebbles by the supposition that they were derived from a
great paleozoic ridge extending northwards towards Cambridge.
* Geological Magazine, No. 195 (New Series, No. 19), Sept. 1880, p. 414.
FOSSILIFEROUS PEBBLES IN THE DRIFT IN WARWICKSHIRE. 485
From this source at an earlier period the Upper and Lower Triassic
pebbles were, as I have inferred, probably derived; and hence it
formed the supply of a large proportion of the Midland Drift in the
districts referred to in this paper. Mr. Etheridge suggested the
possibility of the Wenlock Limestone, lately noticed in a boring at
Ware, dipping to the south. This surmise, Mr. Keeping says, has
since proved to be correct; and therefore a further extension of
ancient Silurian and Cambrian rocks northwards is still more
probable.
This denudation of these old rocks may have come to a close
during the Cretaceous or even some later period, when they finally
disappeared beneath the sea, having been going on for ages, perhaps
commencing at a date somewhat anterior to the deposition of the
Bunter. There are, perhaps, few geological problems more difficult,
to solve than the history (range, distribution, and origin) of these
latest Pleistocene deposits, such as clays, till, gravel, and sands under
the name of Drift, which are so widely spread and often composed of
such heterogeneous materials. Where made up for the most part of
formations present in situ in the immediate neighbourhood or not
very far off, the solution is comparatively easy; but where they
are mainly derived from a great distance, perhaps here and there
from foreign sources, as some of our Midland Drift may be, it is very
puzzling and extremely difficult to determine whence they originally
came and by what means they were transported. Though many
able papers have been written upon this subject, much yet remains
to be done both here and elsewhere before definite and satisfactory
results can be obtained.
[ Note, July 21.—It has since been determined that some of the
Brachiopoda belong to the Caradoc. |
Discusston.
The Presipenr remarked that the subject was a difficult one,
but the species, as stated by Mr. Brodie, were no doubt correct.
At Budleigh Salterton it was easy to tell whence many of the
pebbles had been derived ; but in the Midland counties it was most
difficult.
Mr. Ussuer said that the occurrence of the same fossils did not
prove that the pebbles were from the same area, and that the Drift
of the paper was not quite clear from its title.
Prof. Bonney stated that the author had not expressed this
opinion in his paper; he thought it a most valuable addition to our
knowledge, and was glad that such a contribution had been evoked
by his own slight paper. He thought it almost certain that there
were two sources for the quartzites, and that all the fossiliferous
specimens could not have come from the Lickey, as some had been
found at Nottingham. Probably ancient rocks had extended to the
north-east of England, beyond those discovered in borings at
Northampton, and to the north-east of those exposed at Charnwood.
436 T. M, READE ON THE DATE OF THE LAST
30. The Date of the tast Coance of Leven wm Lancasuire. By
T. Mettarp Reapz, Esq., C.H., F.G.S., F.R.I.B.A. (Read
April 6, 1881.)
In estimating geological time the difficulty always lies in getting a
reliable unit to measure with. Having surveyed and mapped out,
on a scale of 6 inches to the mile, the whole series of Postglacial
deposits between Liverpool and the mouth of the river Douglas, I
have often asked myself, Can the age of any of these deposits be
translated from mere sequence into years? Observation has led me
to believe that an approximation may be made in the case of the
blown sand; and this, as I will presently show, bears upon the title
of my paper.
A reference to the map (1 inch to the mile) and section, figs. 1 & 2,
Fig. 1.—Sketch Map of the Coast at Blundellsands, near Liverpool.
(Scale 1 inch to the mile.) :
SUBMARINE
FOREST ~
il
ALLTEL ir Nw
il
a oF
eee)
-
I
Peat and forest-
bed.
MEASURED
ACCUMULATION
Y) OF BLOWN_SAN ' ts
Boulder-clay.
CHANGE OF LEVEL IN LANCASHIRE. 437
and to those accompanying my paper on the Post-Glacial Geology
of Lancashire and Cheshire, in the ‘ Proceedings of the Liverpool
Geological Society,’ 1871-2, will explain the order and sequence of
the deposits ; and it will be seen that the last movement of the land in
Lancashire was downwards*. Submarine forests at the Alt mouth,
the Rimrose brook, the Liverpool and Garston docks show that sub-
sidence has taken place ; and (which is perhaps quite as good evidence)
sections of stream gullies, cut in the Boulder-clay and filled with
recent silt, at levels far below high water, are frequently met with
in dock-excavations.
Upon the superior peat- and forest-bed, which is an extension
inland of the submarine forests, rests, as on a platform, some 22
square miles of blown sand, in some cases rising 75 feet above
Ordnance datum, and estimated by me to be at least 12 feet in
average depth.
This deposit is shown in my map, as well as in that prepared by
the Geological Survey, by yellow dots; it varies in width at dit-
ferent localities, its maximum being at Formby, where it reaches
3 miles inland. It is quite evident that the whole of this Aolian
deposit is an accumulation subsequent to the last subsidence of the
land ; therefore, if we can calculate the time it must have taken for
the deposit to form, we shall be in a position to determine the least
time that can have elapsed since the subsidence.
The whole of the blown sand has been derived from the shore
between high- and low-water marks, but principally from between
high water of springs and neaps when the shore is dry. On a windy
day it is very curious to see the streaks of sand rushing over the
shore, even when it is damp, shining like rays of a lighter colour
pencilled over a dark ground. The shore is very flat, being in
places more than a mile wide between high- and low-water marks
of spring tides; so that the conditions for the generation of subaerial
sand can hardly ever have been more favourable than they are now.
In May 1866 I set out a plot of land at Blundellsands, in Burbo
Bank Road North, for building-purposes ; it had a frontage of 350
lineal yards to the sea, the western boundary being the then high-
water mark of spring tides. In 1874, for the purpose of enclosing
the said plot, I had to remeasure it to define the boundary, when I
found that high-water mark was considerably beyond the western
boundary, and that the sand had gained upon the sea. An open
wire fence was then put up on the original high-water mark, when
measurement showed that there were 15 yards of land in front of it
at one end, and 5 yards at the other. The high-water mark of
springs had, in fact, receded to that extent. I estimated the deposit
of sand that had taken place in the eight intervening years at an
average of 10 yards wide along the whole frontage and 2 yards
deep. Allowing 1 yard more in depth for sand that may have been
* At Meols, in Cheshire, on the opposite side of the Mersey estuary, was a
Roman station ; and the land is now only a few feet above high-water ; therefore
the land cannot have rzsen since the Roman occupation.
Q.J.G.8. No. 147. 26
438 T, M. READE ON THE DATE OF THE LAST
blown over the top, which I am
convinced is a large estimate, as
very little sand blows on to Burbo
Bank Road North, the eastern
boundary of the plot, we shall thus
have 350 x10x3=10500 cubic
yards of sand deposited in eight
years on a shore-frontage of 350
lineal yards—or 3°75 cubic yards
per lineal yard of frontage per
annum.
Taking this as my unit of mea-
sure (and it is an exceptionally
large one), I find, for the 16 miles
of coast forming the western
boundary of the deposit, it will
give 105,600 cubic yards per an-
num as moved by the wind; and
dividing the 272,588,800 cubic
yards contained in the 22 square
miles, 12 feet thick, it will give
2580 years as the age of the whole
deposit of blown sand if accumu-
lated at the assumed rate.
Since these calculations were
made, I have lately tested their
accuracy in another manner.
There is another plot in Serpen-
tine Road, having a sea-frontage
of 243 lineal yards, and contain-
ing about 6500 square yards.
Serpentine Road was made from
my sections and under my super-
intendence 1n 1866; so that I had
every opportunity of ascertaining
the respective levels. Taking
every thing into consideration, I
estimate that there has accumu-
lated over its whole surface an
average depth of less than 2 yards
of sand (very little blows across
the road); so I think we may
fairly take an average depth of 2
yards as representing the quantity
of sand blown off the shore from
a frontage of 243 lineal yards.
This, extended over fourteen years,
gives 3°81 cubic yards of sand per
lineal yard of frontage per annum.
It is quite evident that the sand
cannot accumulate faster than it
sweeps off the shore; but at other
points on the coast the sea is
(‘depq 00g) ‘paq-3se10y7 outavuqns v se a1oys oy} UO sdveddeoa pue souNp-puKY oY} LopuN senuUIZUOO SIq} YJNOM ITY 04} 4V x
%*
"kelQ Jopfnog,
Highwatermark.
Measured aceu-
mulation of
blown sand.
Dunes.
- Dunes.
The Warren
covered mostly
with dwarf wil-
lows.
Railway.
TL Sla Me gy amy ay7 buopn woyvg—s “Siz
Links of the W. |
Lancashire Golf
Club.
Marsh Lane.
Dunes.
CHANGE OF LEVEL IN LANCASHIRE, 439
gaining on the land ; therefore what is deposited in front of the sand-
dunes is again swept away, and ali that goes to the accumulation is
that which is blown over the tops of the hills or sand-cliffs.
This will also be the case where the coast-line is stationary. —
Again, the high sand-dunes form a barrier that the sand cannot so
readily surmount, the practical effect being that, the bases being
swept by the tide, and the angle of repose remaining constant, less
sand travels inland the higher they grow. At the mouth of the
Alt there is a very extensive bank at low water swept by the north-
west wind ; but the sand does not accumulate, as it is blown into the
river Alt and washed out seawards again. The land on which the
Altear rifle-range is situated has, in fact, as a protection to the river,
been gained from the sea by the erection of artificial obstructions,
against which the sand accumulates. This accumulation has now
practically ceased; and the river and the sea combined are eating
into the land by the Crosby lighthouse, and making sad havoc with
the submarine peat- and forest-bed. :
On referring to the map it will be seen that the blown sand is
narrowest at this point, though the conditions are very favourable
for its development, had the river Alt not intervened.
If, then, it be conceded that the last change of level in South-
west Lancashire was a downward one, I think the facts and cal-
culations I have had the honour to lay before you pretty clearly
prove that it did not take place within the last 2500 years.
Discussion.
The CHarrman (Mr. Hulke) remarked upon the economic as well
as scientific interest of the communication from the proved increase
of land in the area.
Mr, De Rance, who had surveyed the district described by Mr.
Reade in his paper, could corroborate many of the author’s conclu-
sions, especially by the finding of Roman coins on the surface of
the ar land and by a Roman bath only 5 feet above high-water
mark.
Prof. Jupp stated that Mr. Reade’s conclusions were entirely in
accord with the most recent researches concerning the supposed
changes in the level of the shores of the Firth of Forth since Roman
times.
The AvurHor stated that at Hoylake, in Cheshire, numerous
Roman remains belonging to a Roman encampment a few feet
above high-water mark prove that no appreciable downward move-
ment has taken place since Roman times. He thought the actual
period required for the formation of the blown sand was probably
nearer 5000 than 2500 years.
440 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
36. On a new Sprcizus of Piestosaurus (P. Conybearr) from the
Lowsr Lias of Cuarmoutn; with Observations on P. MEGA-
CEPHALUS, Stutchbury, and P. BRacHYcEPHALUS, Owen. By W.
J. Sorzas, M.A., F.R.S.E., F.G.8., &c., Professor of Geology in
University College, Bristol. Accompanied by a SuepLemEnt on
the GrocRAPHICAL Distrisution of the Genus PLEstosauRrus, by
G. F. Wuipzorne, Esq., M.A., F.G.S. (Read May 11, 1881.)
[Puates XXIII. & XXIV.]
Tae nearly complete and very fine specimen of Plesiosaurus
(Pl. XXIII. fig. 1) which forms the subject of the present paper is
the latest addition to the already large collection of fossil reptiles
preserved in the Bristol Museum.
It was found over a year ago, by Samuel Clarke of Charmouth, on
the north-west corner of Blackven Water, half a mile west of the
river Char, where it lay in a ‘“‘table-ledge” of the Lower Lias, some
seven feet above the “ boulder-bed.” From its position and the
species ** of Ammonite still associated with it, we may conclude
that its geological horizon is that of the zone of Ammonites obtusus.
From the pectoral to the pelvic girdle it is imbedded in a layer of
hard impure limestone, thick enough to hold the parts securely
together, but at the same time thin enough to let the skeleton be
seen on both sides, dorsal as well as ventral. The head and neck
were preserved chiefly in shale; so that, to ensure the safety of the
neck, it has been found necessary to imbed it in plaster; but the
head, being filled in and about with limestone, has been left free,
and can be turned about, handled, and examined on all sides.
The ventral surface of the fossil (Pl. XXIII. fig. 1) 1s exposed on
the upper surface of the imbedding limestone; the coracoids lie side
by side nearly in the position they would have occupied in the dead
animal lying on its back, except that they are slightly displaced to-
wards the left side; the left pubis and ischium are also nearly in
position ; but the corresponding bones of the right side have been
pushed to the left, so as to underlie them; the femora, which are all
that is left of the hind limbs, remain on their proper sides, extended
outwards and backwards. The fore limbs have been considerably dis-
placed ; for though that of the left remains on its own side, the palmar
surface of its hand looking upwards, that of the right has been com-
pletely crossed over onto the left, so that its palmar surface would be
directly superposed on that of its fellow were it not for a slight dis-
location at the distal end of the humerus, which has carried the rest
of the right limb backwards, and so left the left hand exposed. The
scapule have turned on their axes, but have not shifted sides; and
* This, according to the determination of Mr. Whidborne, is Ammonites
planicosta,
\
r 2
{
af
.
;
t
S
+
ify
é a ‘
+ 7 .
Quart Journ. Geol. Soc. Vol XXXVILPLXXI.
C Beryean del ot Lith
Minter Broa imp
PLESIOSAURUS CONYBEART.
Mmtern Bros amp .
CONYBEARL AND BRACHYCEPHALUS
So
SUEY
Quart. Journ. Geol. Soe Vol. XXXVIT.Pl XXIV.
PLESIOSAURUS
(g .Berjeau. del et hth.
FROM THE LOWER LIAS OF CHARMOUTH. 441
the “furculum,” or combined clavicles, is tilted up from right
to left.
So far as the appendicular skeleton is concerned, it has approxi-
mately the position it would have in an animal lying flat on its back
with its limbs extended outwards, except that it has been skewed
over as a whole a little to the left, and the right fore limb completely
crossed over.
The axial skeleton is similarly disposed as far as the ribs are con-
cerned ; but the head and vertebral column have been turned round
90°, and lie on one side, the left. The neck and head are also
curved backwards, in the manner so usual with Plesiosaurus, and
which has been commented on by Professor Huxley as suggestive of
death by opisthotonic contraction.
This disposition of the parts of the skeleton may be readily ex-
plained by supposing that the animal to which it belonged fell, after
death, sideways through some depth of sea-water to an oozy bottom.
The body, being broadest laterally, has settled on its back, the hind limbs
sprawling outwards. The left shoulder touched the bottom first ; and
the right fore limb heeling over, fell across the one to the left. The
neck and, in this species, the head being broadest dorso-ventrally,
settled on one side, the left, and so communicated a twisting strain
to the rest of the vertebral column, which, being but slightly attached
to the ribs and appendicular skeleton, readily yielded to it, and
turned on its side also; thus the whole of the vertebral column
came to lie on its broadest face (that is to say, laterally). The twist
to the left given by the crossing of the right fore limb, and the sub-
sequent pressure of overlying strata, led to the various other minor
dislocations and displacements.
That the specimen is undoubtedly the type of a new species is
shown by the following summary of its chief characters :—
1. The length of the skull from the anterior extremity of the
lower jaw to the posterior margin of its articulation with the qua-
drate bone is 19-75 inches, measured along the right side.
2. The number of vertebra is 66, of which 59 are cervico-dorsal,
2 sacral, and 5 caudal. Of the cervico-dorsal vertebrae 38 appear
to be cervical and 21 dorsal.
3. The length of the cervical region is 83 inches (6 feet 11 inches);
so that the length of the head is to that of the neck as 24-1: 100.
4, The length of the cervico-dorsal series is 136 inches (11 feet
_ 4 inches); and the length of the head to this is as 14°6: 100.
5. The length of the centrum of the anterior cervical vertebre is
equal to the height and greater than the breadth of the articular
face. Thus in vertebra xv the measurements are :—Length 2 inches,
breadth 1-5 inch, height 2 inches.
6. In the posterior cervical vertebre the breadth of the articular
face is greater than the length or height, but the latter two dimen-
sions remain equal, Thus in vertebra xxxv we find—length 2:7
inches, breadth 3°5 inches, height 2-7 inches. |
7. The neural spines increase in size up to the 40th to 44th ver-
tebra, in which they measure 4-75 inches in length.
442 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
8. The neural spines are inclined backwards as far as the 55th
vertebra; past this up to the 57th they are inclined somewhat for-
wards; but after this they again incline backwards to the end of the
vertebral series.
9. The humerus and femur are nearly equal in length, the femur
being slightly the shorter.
For the new species which these characters indicate, I propose
the name of Plesrosaurus Conybeart, as a tribute to that classic au-
thority who first made the existence and nature of Plesiosawrus
known to ns. ‘This was sixty years ago; and it is singular that up
to this date no one seems to have thought of calling some species of
Plesiosaurus after the author of the genus.
Plesiosaurus Conybeari agrees closely with P. Htheridgit in the
relative length of head and neck; but if the length of the head be
compared in each with that of the whole cervico-dorsal series, a
marked difference is apparent; thus in P. Htheridgu the ratio is
12°5 : 100, in P. Conybeart 14:6: 100. P. Conybeari further differs
from P. Etheridgu in absolute size, being nearly twice as long; it
also possesses a larger number of cervico-dorsal vertebra, P. Hthe-
ridgw having only 53, or 6 less than P. Conybeari. In this latter
character the new species more nearly agrees with P. homalospon-
dylus, each having 388 cervicals, while the latter has 22 and the
former 21 dorsal vertebree; but P. Conybeart has a larger head ~
than P. homalospondylus. Both haye the same length of neck; but
P. homalospondylus has a longer dorsal series of vertebra (81 inches
in length). The length of its head relatively to that of the neck and
cervico-dorsal series is also much: less than in P. Conybeari, being
to the neck as 10°6: 100, and to the cervico-dorsal series as
04: 100.
Detailed Description.
The Skull (Pl. XXIV. fig. 1).—This, which has been very thoroughly
freed from matrix, and is in an excellent state of preservation, pre-
sents us with that very exceptional character amongst Plesiosaurs, a
good profile. This is due to its having been compressed from side to
side, and not, as is more usual, depressed from above downwards.
Perhaps this indicates a difference in the original shape of the head.
The right side of the skull has slipped a little upwards above the left;
and some other displacements have occurred, but nothing like so great
as one would have expected if the present greatly compressed head
had originally been as broad from side to side as most Plesiosaur
heads evidently were.
Posterior Aspect.—In the middle of the back of the skull is a con-
fused mass of bone comprising the axis and atlas vertebra, under
which the foramen magnum lies concealed. Inferior to this are the
posterior ends (articulare) of the rami of the lower jaws, bent to-
wards the middle line; that on the right side is nearly perfect,
clearly not needing more than a quarter of an inch to complete it.
The articulare thins off rapidly behind its articulation with the qua-
FROM THE LOWER LIAS OF CHARMOUTH. 443
drate, not extending more than 1°5 inch beyond the posterior edge
of the condyle.
The quadrate appears to be directly continuous with the squa-
mosal on each side ; and the latter bones are prolonged upwards into
a process which, viewed from behind, has a somewhat sabre-like out-
line, with the convexity outwards. Both these suprasquamosal
processes are broken at the distal end, so that their junction over the
parietal (a characteristic Chameleon feature seen in most Plesio-
saurs) is not here observable.
Superior Aspect.—Most posterior is the previously mentioned axis
and atlas vertebral mass; then succeed in front the approximated
ends of the broken suprasquamosal processes. The parietal comes
next, a pent-roof-like bone, 5°75 inches long, compressed for the
anterior three quarters of its length into a strong median crest,
along which the persistent sagittal suture extends, expanding ante-
riorly into the foramen parietale 0-3 inch wide, in front of which the
parietal ends. Behind, the parietal is expanded into a form lke
the bowl of a spoon, the bowl being supposed turned with the con-
vexity upwards.
The next bones in front are the frontals, longitudinally ridged in
the middle, smooth at the sides, and separated by a median suture,
which is slightly more open in the middle of its length than at the
ends*. A splintery suture joins the frontals to the nasals, which
are short longitudinally striated bones, not by any means clearly
defined in front from the posterior prolongations of the preemaxille.
The preemaxille, 9 or 10 inches long, are separated for their whole
length by a simple suture; posteriorly they are smooth, or only
faintly wrinkled, but in front much roughened, probably for attach-
ment of integument.
From the parietals a process is given off on each side of the fora-
men parvetale, and continues backwards as far as the middle of the
lateral margin of the bone; in uncrushed skulls this process is a
plate of bone standing out nearly at right angles to the body of the
parietal; its parallelism in this case must be due to compression.
Lateral Aspect.—On the left side the upper jaw is 14°3 inches
long; and the anterior 4°3 inches is furnished by the premaxilla ;
this bone joins the maxilla along a line which runs obliquely
upwards and backwards, to end just above the anterior nares.
The maxilla is an irregularly triangular bone. Its base (10” long)
furnishes the margin of the upper jaw; its anterior side bounds the
premaxilla; its posterior side, just behind the apex, furnishes the
lower anterior boundary to the external nostril, and further down
the lower anterior margin of the orbit (being excluded from the upper
part of it by the lacrymal and prefrontal bones, here badly defined) ;
still further downwards and backwards it meets the jugal, by
which it is excluded from the posterior half of the lower bonndary
of the orbit; and along and beneath this bone it extends to its
* This appears to indicate a fossa corresponding to that on the frontal suture
of the Lizard’s skull, interpreted by Professor Parker as “the scarcely-closed
anterior fontanelle’ of Clarias.”—Phil, Trans. clxx., 1879, p. 598.
444 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
termination, which takes place a considerable distance (over an inch)
behind the orbit. This is a marked character in several of the La-
certilia, particularly the Agamide. The maxilla bears teeth at
least up to within 1-8 inch of its termination.
The jugal is bounded below by the maxilla; in front it forms the
posterior lower corner of the orbit; above it joins the postorbital
(postfrontal), which bounds the upper posterior corner of the orbit ;
and behind it unites with the squamosal by a splintery suture,
which is 1-4 inch long, and runs almost at right angles to the length
of each bone. The jugal is convex outwards in front, and depressed
behind; in the depression a vertical row of three oval pits (nutritive
foramina) separated by intervening smooth ridges is situated. At
the ends of the pits, which are elongated antero-posteriorly, strize
appear on the surface of the bone, and are continued forwards,
diverging at the same time, over the otherwise smooth anterior con-
vexity. The external form and surface-markings thus described
give to the jugal such a characteristic appearance that it is easily
identified by them alone.
The squamosal is a large and important bone, of which the
general form and relations are not quite so clearly defined as could
be wished. Its characteristic anterior or zygomatic process, how-
ever, is well displayed; it is a thin bar of bone 1 inch broad, about
23 inches long, and + inch thick, finely striated longitudinally, the
strize sweeping somewhat obliquely forwards from above down-
wards.
The postorbital continues backwards from the jugal over the
upper edge of the zygoma for a distance of 0°8 inch. These three
bones, Jugal, postorbital, and squamosal, clearly meet in a T-shaped
suture; and thus Professor Huxley is undoubtedly correct in assert-
ing that, “‘ contrary to what is usually stated, the postfrontal appears
. to articulate with a bone, the homologue of the squamosal
of the Crocodile” (Quart. Journ. Geol. Soc. vol. xiv. p. 293).
A slight extension downwards of the lower margin of the anterior
end of the squamosal bar, rendering its inferior outline curved con-
cavely, while that above is rectilinear, brings it within half an inch
of the posterior end of the maxilla. From that part of the jugal
which is exposed between the squamosal and the maxilla no bony
bar is produced towards the quadrate; nor is there the slightest
evidence of one having ever existed, so far as this skull is concerned.
I feel persuaded that an inferior bony temporal arcade has never
been present, and that, if a quadrato-jugal occurs at all, it must be
as what we have called the anterior process of the squamosal, while
for such a view I see no evidence.
The quadrate is clearly enough identified at its articulation with
the lower jaw; but on tracing it towards the squamosal it is impos-
sible to say where it ends or the squamosal begins. The relations of
the two bones are quite obscure; so that one cannot even tell in this
specimen whether what we have already termed the suprasquamosal
processes are the property of the bones to which we have assigned
them, or whether they came off from the quadrate. They appear in
FROM THE LOWER LIAS OF CHARMOUTH. 445
other skulls, however, as continuations of the squamosals, though
apparently divided from them by suture. Owen calls them “ supra-
mastoids ;” and they may correspond to Parker’s ‘‘ second supra-
temporals,” though, as they lie exterior to the squamosals and not
beneath them, our term ‘“‘ suprasquamosal” is perhaps best retained.
The articular end of the quadrate lies much below the general
level of the upper jaw (over an inch). This is a character not found
in Agamide or most Lacertilia; but it occurs in Iguana and the
Chameleons.
The Lower Jaw.—This, which has the usual reptilian composition,
is 20°35 inches long from end to end; posterior to the symphysis its
surface is smoothly striated by longitudinal thread-like ridges, the
external expression of its fibrous structure ; in front, past the pos-
terior end of the symphysis the surface is much roughened, and
along the alveolar margin finely wrinkled*. The length of the
symphysis is 3°35 inches; the height of the jaw from the top of the
coronary to the lower margin of the ramus is 3 inches.
In the following Table are given the more important measure-
ments of the skull :—
inches.
Anterior extremity of preemaxilla to posterior margin of parietal......... 18:0
Bs yp anterior mar gin OO, Gocenooucoos 10:0
- posterior margin of orbit ............ 13-0
Ks a Bi left nostril ...... 8:2
Le s s right nostril 9:2
a Ys foramen’ parietale .-2%.25..2.0+.----0¢ 13-0
Worn nereht of orbit ie SEGRE ase tO ota Sota cars dale ameetacucaeecagesaes 3:2
8 TaTELINS: “nerd SOaecaeheis eae Re Se eer On 21
Highest point of parietal to lower margin of lower jaw i ea eee ce
Anterior end of dentary to posterior margin of articulation with quadrate 19°75
3 x posterior end! of articulare) <..2:..<0.02..5:..c<00s 21:0
Section across the Skull—The skull has been broken across in
several places, so as to afford a view of its internal structure; but
very little is clearly displayed, except in the most posterior fracture,
which traverses the supratemporal fosse (fig. 1, p. 446).
A large and originally bilaterally symmetrical mass of bone is
seen in the middle of the section above the lower jaw; the greater
part of it consists probably of the basisphenoid ; it is channelled in
the middle line above by a deep narrow groove, through which a
line can be drawn to the middle point of the inferior concave margin
opposite, dividing it into nearly symmetrical halves; the right moiety,
having apparently suffered but slightly from compression, is better
fitted for study than the left, which is much crushed together. The
right half is divided by a deep lateral excavation into an upper and a
lower portion : the latter, descending outwards and downwards, soon
bifurcates; and the upper of the two processes so produced, after
diminishing to a narrow neck, widens suddenly into a triangular
* The wrinkled appearance here referred to is very similar to that exhibited
by parts of the integument described on page 466.
446 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
area, the transverse section of a bone which is continued backwards
on the side of the skull to terminate on the inner side of the lower
end of the quadrate. In all probability this bone is the pterygoid, or
Fig. 1.—Transverse Section through the Skull in the Region of the
Supratemporal Fosse, (Scale 5.)
at all events a part of it; and the narrow neck from which it extends
may be partially furnished by the basipterygoid process ; but there is
no evidence of the existence of a joint between it and the pterygoid.
The lower process of the bifurcation may also be a part of the ptery-
goid; if not, I do not know what nature to suggest for it.
On the left side the pterygoid is crushed up against the basisphe-
noid, almost obliterating the space which separates them on the
right; and the descending process below it is thrust and broken
against the lower jaw.
FROM THE LOWER LIAS OF CHARMOUTH. 447
On each side of the section above the basisphenoid the thin bar
of bone which proceeds from the squamosal is seen, and at the
summit the parietals with their median crest and persistent suture.
The other bones appear to be undeterminable ; some of them are
probably parts of the periotic mass.
Dentition.—A fine series of teeth is well displayed on the left side
of the head. They are slender, conical, slightly recurved, and finely
striated from the apex for a considerable distance downwards, 2. ¢.
over the crown. They vary greatly in size, the largest being those
in the neighbourhood of the maxillo-premaxillary suture; an inch
or so behind this they begin to diminish in size, and beneath the
orbit have less than one half the average length of those in front,
while behind it they dwindle to mere pointed tubercles.
The largest tooth present is one in the right upper jaw, behind
the maxillo-premaxillary suture; it is 2°45 inches long, the distal
1°5 inch, or crown, finely striated, its diameter at the point where
the striz begin being 0°6 inch. A smaller but more perfect tooth,
the largest on the left side, measures 1-95 inches long; 1°35 inch is
striated ; and the diameter at the commencement of striation is
05 inch.
Those teeth which still remain exposed to view are distributed as
- follows :—on the left side in the premaxilla 5, in the maxilla 15,
in the lower jaw 13; on the right side in the premaxilla 3, in the
maxilla 11, in the lower jaw 8. The number of teeth in the left
premaxilla and maxilla make the nearest approximation to the
numbers originally present.
The Vertebral Column.—tThere is a continuous series of 66 ver-
tebre, of which 38 are cervical, 21 dorsal, 2 sacral, and 5 caudal.
The caudal series is evidently incomplete, a considerable number of
vertebre being missing from the distal end.
Cervical Vertebre.—The first and second, as already mentioned,
form a confused mass adherent to the back of the skull, but from
the third onwards all are clearly defined and can be easily examined.
m1. The centrum of the third is 1:12 inch long* (a.p.), 0°75 broad
(1.1.), and 1:4 high (d.v.), the breadth and height being measured
along the articular face. It is much compressed in the eaiddle, the
edges of the articular ends projecting greatly, as though the more
yielding cancellous interior had given way under heavy pressure,
such as that of overlying strata; this feature is markedly present as
far as the thirteenth cervical vertebra. ‘The neuro-central suture is
a nearly straight or slightly tricurvate line, with the central con-
yexity downwards. A tricurvate ridge, with the central convexity
upwards, runs along the whole length of the centrum between the
articular edges or rims, at a level 0-4 inch below the neuro-central
suture; it defines the upper edge of the nearly oval costal pit, which
is 0-9 inch long, 0:45 inch broad (d.v.), and obscurely divided into
two by a faint median longitudinal ridge or closed furrow. The rib
has been displaced downwards; and its ovate-lanceolate posterior
* (a.p.) antero-posterior, (l.1.) from side to side, (d.v.) dorso-veutral.
448 PROF, W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
prolongation extends with a downward direction as far back as the
posterior edge of the centrum to which it belongs.
Near the articular ends the centrum is roughened by a few small
irregularly scattered tubercles, which become larger and more nume-
rous in succeeding vertebra down to the twenty-fifth. The neural
spine has been broken away ; so that the total height of the ver-
tebra cannot be determined. The line between the zygapophyses is
1°9 inch from the base, and 0:9 inch from the neuro-central suture.
vu. The seventh vertebra has a total height of 2°95 inches; the
centrum is 1:°375 inch long and 1°5 high. ‘The well-marked neuro-
central suture is 1-1 inch from the base. The tubercles near the
articular ends have become larger and more numerous. The rib is
distinctly hatchet-shaped, and consists of a blade-like upper part and
a lower handle-like horizontal process ; a deep incision separates the
handle from the blade in front, and the front end of the handle does
not reach the anterior edge of the centrum by about an inch. ‘The
posterior margin of the blade slopes gradually down, and curves
gradually into the handle, the posterior prolongation of which ex-
tends a short distance beyond the posterior edge of the centrum,
from which the rib proceeds.
The anterior zygapophysis is, as in the other anterior cervical
vertebree, turned inwards and upwards; below the line of the zyga-
pophyses the neural arch is ridged in a direction crossing obliquely
from the anterior edge of the anterior zygapophysial facet down-
wards to the posterior edge of the neuro-central suture, the ridges
being most marked near their origin and termination. The distance
from the anterior to the posterior zygapophysis is 2°3 inches. From
the line of the zygapophyses to the base of the centrum is 2°0 inches,
to the top of the spine 1°35 inch.
The neural spine has somewhat the outline of a Phrygian cap seen
in profile; it has a gentle convex slope backwards in front, and a
short sigmoid curve behind; it rises from the middle of the length
of its centrum, and hangs over the anterior quarter of the centrum
next behind. It is smooth below, but roughened towards the distal
end.
The vertebre increase in size and change in the relative size of
their parts as they pass backwards: down to the fifteenth (xv), pro-
bably to the twenty-second (xxir), the articular face of the centrum
is an ellipse, with the major axis vertical (d.v.); at the twenty-third
(xxur) the diameters are about equal, and continue so to about the
twenty-fifth (xxv), beyond which the horizontal diameter (1.1.) be-
comes the larger, and continues to increase over the vertical down
to and beyond the end of the cervical series. The neuro-central
suture becomes more sharply inflected in the middle, so that in the
fifteenth (xv) the middle curve of the tricurvate line becomes trans-
formed into a right angle. The zygapophysial facets acquire by
degrees an entirely horizontal position ; they seem to have done so
in the fifteenth vertebra.
The neural spines increase more rapidly in size than the centra,
and considerably change their form; at the eighteenth (xvm) the
FROM THE LOWER LIAS OF CHARMOUTH. 449
spine is broader at the distal end than in the preceding vertebra.
The anterior margin is short and straight, sloping backwards;
the upper margin curved, rising obliquely backwards; the posterior
margin is sigmoid, convex backwards above, and concave below,
nearly vertical. In the thirty-second (xxx1r) the outline is much
sunpler: both anterior and posterior margins are straight, not quite
parallel with each other, since they are further apart below than
above; the upper margin is an elliptical curve, through which the
anterior and posterior margins pass into each other. The base of
the anterior part of the spine between the anterior zygapophyses is
much compressed ; it broadens out immediately behind the origin of
the anterior zygapophyses, and also over the posterior zygapophyses.
The costal pits increase in size; but neither they nor the ribs show
much sign of other change down to the twenty-sixth (xxvI) ver-
tebra, when, however, preparations for change become evident.
In the twenty-sixth, the rib being displaced allows the costal pits
to be seen ; they are now quite separate oval depressions, 0°95 inch
long and 0-9 inch distant from the anterior edge of the centrum, with
which they are connected by a ridge which continues the anterior
margin of each forwards.
In the twenty-seventh (xxv) all trace of rugosity has disap-
peared from the surface of the centrum, and it is now quite smooth;
this continues to be the case throughout the rest of the vertebral
column. The neuro-central suture is marked by a swelling ridge,
particularly prominent in the central part of its course.
In the twenty-ninth (xxrx) the thickening of the lower end of
the neural arch becomes more marked, and the margin of the costal
pits is somewhat elevated.
In the thirtieth (xxx) faint signs appear of a ridge proceeding
from the swollen end of the neural arch to the upper margin of the
costal pit; in the thirty-first (xxx1) this and the ridge connecting
the anterior margin of the costal pit with the anterior edge of the
centrum have both become more marked. In the thirty-second and
thirty-third (xxx and xxxi11) the costal pits begin to rise higher
on the centrum, and become more posterior ; the upper edge of the
pit swells into a marked ridge, and is connected by the previously
mentioned ridge, which (now become very prominent) ascends from
it to the swollen end of the neural arch.
In the thirty-fourth (xxx1v) the lower costal pit has almost dis-
appeared, and the upper and anterior margins of the remaining pit
are swollen into a strong crescentic ridge, which is joined in the
middle by the ridge descending from the neuro-central suture.
In the thirty-fifth (xxxv) the thickened lower end of the neural
arch and the ridge arising from the anterior margin of the costal
pit form together a single vertically descending median ridge, which
extends more than halfway down the side of the centrum. That
part of the ridge contributed by the neural arch is more swollen
than the other, and curves forwards as it descends, joining at an
obtuse angle the part contributed by the centrum, which is sigmoid
in outline ; the general form of the united ridge is much like that
450 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
of a bracket (}), the middle point of the bracket standing for the
point of junction of the two constituent ridges.
In the thirty-sixth (xxxv1) the lower end of the neural arch is
still more swollen, and has retreated further up the centrum; it
more abruptly joins the costal ridge, which has become almost
straight, and more prominent; it extends down the middle of the
centrum to within 0°65 inch of an oval nutritive foramen, which lies
on one side of the concealed middle line of the base of the centrum.
(xxxvi1) An abrupt change in the character of the costal ridge
takes place in the thirty-seventh vertebra; it has become greatly
enlarged, to form a simple transverse process, which, curving down-
wards and backwards from the neural arch, ends in an oval facet,
looking obliquely backwards and downwards; the lower edge of the
facet rests upon the centrum, the pedicel of the transverse process
having as yet only an upper and not an inferior margin. The rib
is no longer hatchet-shaped, but of the ordinary half-hoop form ; it
is nearly cylindrical down to 1:3 inch from the transverse process,
and then expands laterally so as to become somewhat triangular in
section ; the line along which this change takes place is marked by
a strong ridge, oblique to the axis of the rib. A transverse fracture
across the front of this vertebra and the overhanging posterior zyga-
pophyses of the preceding vertebra shows that the zygapophysial
facets are not horizontal (as one might have conjectured), but much
inclined, the posterior looking outwards and downwards, and the
anterior inwards and upwards.
(xxxviit) The base of the transverse process of this vertebra ex-
tends a little more than halfway down the centrum; the facet is
borne on a distinct pedicel, and looks a little less backwards than
that of the preceding vertebra. This I take to be the last cervical
vertebra, the transverse process of the next vertebra appearing to
arise wholly from the neural arch. I use the word ‘“ appearing”
definitely, since, in the absence of any well-defined neuro-central
suture, it is difficult to say certainly what the exact constitution of
the transverse process is. It is clear, however, that the process in
this vertebra extends a little below the dorsal half of the centrum ;
and this is presumptive evidence* that it is cervical; while in the
next vertebra it does not, but is wholly confined to the dorsal half,
and thus should be the first dorsal. Moreover, owing to a difference
in the colour of the substance of the centrum and that of the neural
arch, the latter being black and the former brown, in this region of
the vertebral column, it is possible to detect in the transverse pro-
cess of the thirty-eighth vertebra bone contributed by the centrum ;
in the transverse process of the thirty-ninth no certain indication
of bone so contributed is to be found. The possession of hatchet-
shaped ribs was at one time included by Professor Huxley in the
definition of a cervical vertebra ; if this should be regarded as an essen-
tial character, then the vertebre thirty-seven and thirty-eight would
* «There is reason to believe that the neurapophyses do not extend upon the
bodies of the cervical vertebree beyond their dorsal half.”— Hux.ey, on Plesio-
saurus Ktheridgit, Quart. Journ. Geol. Soe. vol. xiv. p. 282 (footnote).
FROM THE LOWER LIAS OF CHARMOUTH. A51
be excluded from the cervical series, and there would be only thirty-
six cervical vertebree. If it were desirable to make a natural group-
ing of the vertebre of this skeleton without reference to those of
other species, one would not hesitate to draw the line between cer-
vical and dorsal at the end of the thirty-sixth vertebra; for all
down to the thirty-sixth are without transverse processes, but pos-
sess hatchet-shaped ribs, while past the thirty-sixth the hatchet-
shaped rib disappears and unmistakable transverse processes corre-
spondingly arise. As, however, it is convenient to adhere as closely
as possible to existing conventions, in order to facilitate the com-
parison of species, I have been governed in my determination of the
last cervical by the fact that a part of the transverse process borne
by it does clearly seem to be contributed by the centrum as far back
as the thirty-eighth vertebra; and thus I have included as cervical two
vertebree which would certainly seem more in place in the dorsal
series. Professor Seeley’s plan of calling those vertebre in which
the transverse process is passing from the centrum onto the neural
arch “pectoral” has much to recommend it, and might fairly be
applied to the vertebree thirty-seven and thirty-eight. Indeed there
is just a shade of doubt in my mind whether vertebra thirty-nine
should not also be called pectoral; for its transverse process appears
to havé a little brown bone like that of the centrum at its base,
and the rib it bears is bifurcate near the head and short, while the
succeeding vertebre bear ribs with a simple proximal termination
only.
The determination of the position of the last cervical vertebra is not
only important as giving us the number of vertebre in the neck, but
also because it furnishes us with a necessary datum for the measure-
ment of the length of the neck, and hence for ascertaining that im-
portant character, the ratio of the length of the head to that of the neck,
or, as we may briefly term it, the cervico-cephalic index. Fortunately,
in the case of the species under consideration the neck is so long that
one or two vertebree more or less can make very little difference to
the value of this index, the thirty-seventh and thirty-eighth vertebre
measuring together not more than five inches. The thirty-eight
cervical vertebree measure 83°25 inches, or 6 feet 11 inches; and
the cervico-cephalic index is 24:1. A Table is here appended,
giving the dimensions of the cervical vertebrx, so far as they are
ascertainable: it will be seen that the constancy in length which
Prof. Owen* regards as characteristic of the cervical vertebra of -
the Enaliosauria, and only exceptionally absent in Phiosawrus, has
no real existence, and also that no single vertrebra can well be taken
as typical of the remainder. Hence the importance of such a Table
as this as a help in the specific identification of separate vertebre
will be apparent. It may be worth while to call attention to the
abrupt manner in which some of the changes in dimensions occur, as
for instance in the length of the centrum in passing from the twenty-
second to the twenty-third vertebra; and again, to the abnormal
* Report Brit. Assoc. 1841. Report on British Fossil Reptiles, p. 63.
452 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
variations which occasionally appear, as, for instance, in the twenty-
eighth vertebra, which is longer not only than its predecessor, but
also than its successor; the same is also the case in the thirty-sixth
vertebra: the difference is too large to be explained as an error of
measurement, and can scarcely be the result of mechanical compres-
sion; it seems rather to be concomitant with that wide departure
from the ordinary Reptilian type which the Plesiosaurian neck
Or
On
pin
Sir O1
2°3
24
NOW No ot a NG)
on
on
= DO DMDDOMDADA”B
rN)
(oP)
on
oS
b>
> ConA
Or
Ov Or Or OURS 9
oO
6:4
Oo WITHA
creo bo:
Our
Or
a
o9
aS
on
2-45
Ovo
presents.
Table of Measurements of Cervical Vertebre.
Centrum. Zygapo- | Zygapo- | 2Y82P0- | Neuro- eae
a pie | Total | Physis | physis payeis cone suture Noe
WO een || iitole toiendl suture |
vertebral], ength.| Breadth.| Height.) “5 base. | of spine.| ZY84P0-| _ to costal | Vertebra.
(a.p.) (1.L.) (d.v.) physis. | base. pit.
Ih
2.
3 12 | 0°75 1-4 1:9 12 0-4 3
4, 25 Sass 1:4 1E9 21 Teal 0-4
5 295 1:4 2:0 1:35 1-1 0:4 9)
6. 375 14 29) 2:0 ; 2°3 11 0:5
7, 375 15 2°95 2:0 : 2°3 1-1 0:5
8. 3795 15 2°95 2:0 1:45 2°3 11 0-5
9. "379 15 32 2:0 2:3 11 0:5
10 (i 15 2:25 2-45 | 1:05 | 0°5 10
11 7 ey 2:3 ravasd) | 11) 0-5
12 7 1-4 1-7 2°45 0 12 0-5
13 8 145 | 1°75 2:45 14 | 05
14 9 14 19 2: 1:9 1-4 0-5
15 0 15 20 4-0 2:1 275 | 1:5 0-6 15
16 ‘il aoe 2-1 4-6 2:2 2:35 | 1:55 | 07
17 2 2-1 4:8 2°45 3°05 | 1:55 i
18 2 2°2 oul 2°45 3°05 | 1:5 a
19 2 2:2 5:2 1
2 2: 5:4 2°8 1 20
2: 1
2° 1
2 1
2 2
2
9.
9.
Ds
2
DOA2WS
Do
or
I-10
On
Oo: TOUT: H HS bS
Or
©
a
qoceto. ewe. wee
WDA HOH
(30)
oo)
or
Soo qoacoe SIOSoeooe
bo
S
DPN NHWNNNYNNNNYNNNNNNNNNHE REE eee ee eee
DS Or Or So
Oo Sod Or
bo Cr
Or
AINA ATID DOO
TCH OD HE OO 00 CO St
3 2:7
35. | 269 | 3 2°8 wah 30.
3 28
yt
2 G9 9 C9 CO OO CO G2 U9 G9 U9 C9 CO CO OD DD DD LO DO LOND bb
100 GO Gd =a
a
aS
Dent my 38
FROM THE LOWER LIAS OF CHARMOUTH. 453
Dorsal Serves. (Plate XXIII. fig. 2.)
The dorsal vertebree are well exposed ina fine and complete series
on the underside of the specimen. ‘They have the same general
character as the last two cervicals—the centrum being smooth, not
tuberculated, its height (d.v.) and length (a.p.) being about equal,
and both shorter than the breadth (1.1.). The maximum dimensions
of the centrum appear to be attained in the fortieth vertebra, in which
the length and height are each 2°8 inches, and the breadth 4:8 inches ;
its total height, however, is only 7:6 inches, being less than that of the
forty-third vertebra, which is 8:2 inches high ; behind the fortieth the
centra decrease in size, and a little more rapidly in breadth than in
the other dimensions. ‘The transverse processes rise upon the verte-
bre from the thirty-ninth (xxxrx) to the forty-second and forty-third
(xLII and xt1r) beyond which they spring from the neural arch along
the zygapophysial line ; they maintain this position down to the fifty-
sixth (Lv), past which they begin to descend and also change in
character. At first, as in the fortieth vertebra (x1) or second dorsal,
the pedicel of the transverse process projects outwards at right angles
to the vertical plane given by the flat side of the neural spine;
passing backwards this angle is much diminished, so that in the
forty-fourth (xxv) vertebra it is only 65°; behind this it begins to
Increase again, and at length becomes 90° at the fifty-fifth (Lv)
vertebra, or seventeenth dorsal.
The length of the transverse process increases slowly down to the
forty-seventh (xivir), in which it is 4-3 inches long; behind this it
slowly shortens and becomes 1:5 inch at the fifty-eighth vertebra.
The dorso-ventral diameter of the base of the transverse process
is at first, as in the fortieth vertebra, 2-1 inches; but it rapidly
diminishes, so that at the forty-third it has become 1:2 inch;
past the forty-third it remains pretty constant as far as the fifty-
sixth vertebra. At the fifty-sixth important changes commence ; the
transverse process loses its straight boldly projecting form and droops,
as it were, into a curve, assuming the character of the last cervical
transverse process. In the fifty-eighth vertebra the facet is inclined
downwards and backwards ; but its form cannot be fully made out,
as its lower half is concealed by the head of its rib.
The neural spines are parallel-sided, and truncated above by a
straight or very gently curved distal margin. They attain their
greatest length and breadth in the fortieth to forty-third vertebre,
past which they diminish in size slowly. In the early part of the
dorsal region the spines are inclined backwards at a slight angle ;
thus in the fortieth to forty-second vertebre the axis of the spine
makes with the zygapophysial line an angle of 64°, 2.¢. it slopes
backwards 36° from the vertical ; posteriorly the backward inclina-
tion diminishes and the spine becomes at length vertical; this is the
case at the fifty-fifth vertebra ; still more posteriorly the inclination
becomes reversed and the spine slopes forwards; thus in the fifty-
seventh vertebra it makes an angle of 93° with the zygapophysial
Q.J.G.8. No. 147. 25
454 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS.
line, 2. ¢. itis inclined forwards at an angle of 3° from the vertical ; at
the sixtieth (Lx) vertebra (1st sacral) the spine has resumed its
backward inclination. -
The fabs.
The early dorsal ribs for about two inches from the proximal end
are almost straight ; they then somewhat rapidly bend into a curve,
which is steeper near its origin and straighter towards the end. At
the fifty-first vertebra the curvature of the rib has become less, in
the fifty-third much less; and at the fifty-fourth the rib is straight.
The longest ribs are those of the forty-seventh to the fiftieth ver-
tebre ; behind the fifty-second they rapidly shorten, those of the
fifty-sixth being only 5:4 inches, and of the fifty-ninth 2-7 inches
long.
For a short distance from the head the ribs are roughened with
irregular longitudinal ridges, which are most marked in the anterior,
and absent in the last few posterior dorsal ribs. All possess simple
proximal ends, except the first dorsal, which gives off a short process
just below the head.
Sacral Vertebre.
The two vertebre regarded as sacral are the sixtieth and sixty-
first (Lx and 1x1). In them the transverse process has become very
short, little more than a raised facet, the surface of which, however,
is larger than that of the preceding transverse process of the last
dorsal. It obviously consists of two nearly equal parts—an upper
contributed by the neural arch, the articular face of which is a plane
surface, meeting along a horizontal line at an obtuse angle the
similar plane surface of the inferior moiety contributed by the cen-
trum. ‘The ribs are short (1:9 inch long) and slightly expanded
at the distal ends. The neural spines are inclined backwards, making
in the sixtieth an angle of 80°, and in the sixty-first of 78°.
Caudal Vertebre.
If the determination of the sacral vertebree be correct, then there
are five caudal vertebrae, the dimensions of which are given in the
appended Table (page 455) of measurements for all vertebree past the
last cervical. The spines are broken away from them all except the
first, in which it is suddenly inclined backwards at a much greater
angle than that of the last sacral. The zygapophyses are nearly
vertical. .
The transverse processes are now represented merely by pits with
raised margins, only the upper part of which is furnished by the
swollen end of the neural arch. The ribs remain short; but that of
the first is longer than that of the last sacral.
Table of Measurements of Postcervical Veriebre.
. __|Inclina- a 3B
Length | Length |Inclina- Peo ouapes
Nor Centrum. ay | | pve et © of tion of pa Honeth & i S gq = a
oem Total | @Y ee P- | to end | a ip of |2nterior| spine | spine Bes Length fae 6 8 vs a8 a ae
height. of ae margin} along to of rib. epee De :
tebra. base. spine, | 2782P- | spine. of middie line of | Proves verse BF 4,8 verse
Length. | Breadth.| Height. spine. | line. | zygap. ee Process: He cao See BCs a
es pe eS 5 are ie oe eee eee
in. in. in. in. in. in, in. in. in, in. . 5 in. in. in, in, in
39. 2°6 3D 2'8 ae 4:2
40. 2°8 4-1 2:8
et et
SvSr Or Or Ot
Pt et tt tt tb
ell \2 Meal NO We NO SUC Os
8
OLS ~ SiS
Med DOMOODOMED DOO
OU ON
SCHWNHHARAAMWOWNNH OO
°
Over
Or
Or or
on
=
eo
fon)
ES °
oo
Or
Ye)
S
We)
S
a
°
—
a
On
(e2)
j=)
-J
oe
—
=
ler)
H FOU SIS GO CO CO OE HO DY CO WONT Oo OVO
.
°
Ourcr
WMOH Odo WH OHOH
M09 00 Gir:
oO
to
bo
>
iw)
bo
Or
bo
tt et pt
456 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
Pectoral Arch.
The bones of the pectoral arch are all present, though somewhat
displaced from their original position. They consist of the furculum,
coracoids, and scapule.
The Furculum.
This (fig. 2) is a large bilaterally symmetrical plate of bone, convex
ventrally from side to side, with two long thin tapering lateral wings,
one on each side, directed backwards and slightly dorsally; a tri-
curvate anterior margin, the central curve being a large semicircular
excavation, which passes into a curve convex forwards on each side;
and a gently curved posterior margin convex backwards, with a
narrow deep incision running forwards along the median line, or
axis of symmetry. The lateral curve of the anterior margin passes
insensibly into the front margin of the lateral wing; the posterior
margin meets the posterior margin of the wing in a rounded
angle.
Fig. 2.—Diagram of the Furculum. (Scale 3.)
\
he
If one draws a line from the central point of the curve, which we
have just called a “ rounded angle,” parallel approximately to the
anterior margin of the bone, we shall divide the body into two parts,
the anterior of which is much thicker than the posterior, being at
least 1 inch across ; it is of somewhat dense or close texture super-
ficially, but loose and open in the middle: the posterior part is very
thin, a mere lamella of bone. The anterior part may be distin-
guished as the ‘‘ body” proper of the bone; the posterior, which is
divided into two by its median longitudinal fissure, is a pair of
“lapels;” and thus with the “wings” we have five distinct re-
gions present, but of true sutures I cannot find a trace; the whole
appears to be a single piece of bone, though having regard to the
great difficulty there often is in discovering sutures which do really
exist in fossilized bones, I should not wish to be thought too posi-
tive on this point.
The bilateral symmetry of the bone and its median longitudinal
FROM THE LOWER LIAS OF CHARMOUTH. 457.
notches, point to its connate nature; its position in front of the
coracoids, between the prescapular processes of the scapule, points
to its clavicular origin: I regard it therefore as representing a pair
of fused clavicles, which repeating the behaviour of the coracoids,
have expanded into extensive plates over the ventral surface. An
interclavicular element appears to be absent; there is no room for it,
except in the position conjecturally assigned to it by Protessor
Seeley, who has suggested that it forms the anterior middle part of
the bone. This, however, is a position which it occupies in no other
known reptile, as it is always more or less posterior instead of an-
terior to the clavicles. Since writing the first part of this paragraph
I have been able to devote a few minutes to an examination (which L
wish could have been less hasty) of a loose specimen of Plesiosaurian
furculum, preserved in the British Museum, the same bone, I fancy,
that is figured as a sternum in Hawkins’s monograph. It certainly
shows traces of sutures, and is marked on the surface by strive, which
appear to indicate a median and lateral elements. It has a suggestive
resemblance to the clavicles and interclavicle of a Chelonian like, say,
Trionyx. But it differs considerably in form and appearance from
the furculum of our species ; so that it is doubtful how far it can be
used as a guide. Very possibly the furcula of different Plesiosaurs
may differ in composition, as they do in Birds, an interclayicle being
sometimes present and sometimes absent.
There is another difficulty attending the interpretation of the fur-
culum ; and that lies in its position beneath the prescapular ends of
the scapule, which overlap its posterior lapels. In all recent rep-
tiles the clavicles are superficial to the scapule, while here just the
reverse is the case. ‘This is proved by more than one well-preserved
specimen in the British Museum, showing the scapular processes
abutting on the body of the furculum, and also by Lord Enniskillen’s
specimen of P. macrocephalus, which affords us a dorsal view of the
left clavicle overlapping the dorsal surface of the scapula (fig. 3).
Fig. 3.—Diagram showing the lefi side of the Pectoral Arch of
P. macrocephalus, seen from behind. (The wing of the furculum
conceals the termination of the scapula.)
458 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
This anomalous position I altogether fail to explain : if the lapels
could be shown to be precoracoids, all would be clear; but this view
is not without difficulties.
The dimensions of the bone are given below :-——
inches.
Antero-posterior diameter in the median line
(GS, 5. BAD)» 66-006 3°65
Maximum antero- -posterior diameter (ib. ¢ dl) 6-4
Antero-posterior diameter from a tow...... 5°25
Breadth) (Gwaceitheslimeti)) eae er eee 8:6
Length of wing (g h).. BU SEES eek nO ee
Width of anterior excavation (¢ 9g) prance 2°55
Depth of anterior excavation (av) ........ 1:05
Depth of posterior incision .............. 2a
The Coracords.
The coracoids (fig. 4) have the usual Plesiosaurian form, presenting
together a close and almost ludicrous resemblance to the front of a
short jacket.
Fig. 4.—Diagram of the Right Coracoid. (Scale 3.)
The inner margins of the bones meet for half their length in a
straight median harmonia, diverging gently outwards from each end
of it. The outer margin has a simple concave sweep backwards
behind the articulation for the humerus ; the anterior margin pro-
jects in an elliptical curve in front, the outer edge of the curve sink-
ing into a curve backwards, which joins the almost straight margin
of the scapular articulation. The bone is thickest where it furnishes
the articulations for the scapula and humerus. Thence it continues
with only slightly diminished thickness along a ridge or keel, which
extends transversely to its inner margin. This ridge, which rises
from the ventral surface of the bone, and as shown by a transverse
FROM THE LOWER LIAS OF CHARMOUTH. 459
fracture, is scarcely, if at all, marked on the dorsal surface, is de-
fined in front by a curved line, which commences near the anterior
end of the scapular articulation, curves backwards to the middle of
its course, and then forwards till it ends against the inner margin of
the bone; posteriorly it is defined by a line very slightly curved,
convex backwards, which commences from the hinder end of the
humeral articulation and passes very slightly backwards, also to end
against the inner margin. From this ridge the bone thins rapidly
away in front and behind, more rapidly in front, till it ends in a
thin edge.
The posterior region of the right coracoid is traversed by several
lines of fracture, on one side of which the surface of the bone remains
higher than on the other, and thus forms little cliffs. A broken sur-
face, dividing the bone across, reveals its internal structure, and shows
between its dense outer layers a more cancellous open tissue in the
middle ; not only so, but in some places the middle of the bone is
occupied by a layer of calcite; and this is thicker on that side of a
fracture where the surface is higher, and thinner on that side where
it is lower. This calcitic layer is probably due to the replacement
of cartilage ; and it is thinner where the bone is thinner on the side
of a crack, because the cartilage had there been squeezed together by
pressure of overlying strata.
The measurements of the right coracoid are given below :—
inches.
Maximum length (fig. 4, mxv)............ 17:375
Henethvot harmonia Gb: @p) ............. 10°5
EBenea chee ens?) Nea c0-) she iced Seles Siete esses 86
Breadth along median ridge (1b. hr). sox!)
Distance from anterior end of coracoid to
posterior edge of glenoid cavity (ib.mt).. 10:0
Length of chord of anterior concave margin
of coracoid (ie FOG)! ane hoe 2°75
Height of are of anterior concave margin of
EOLACOrdG (Tb fi) is ah uals ed. ifn se. A 0°375
Length of articulation for thescapula(ib.ds) 3°3
Length of articulation for the humerus(ib.s¢) 3°2
Thickness at articulation for the humerus.. 1°6
Length of chord of posterior and outer lateral
ATEVO (Os G2) Ae eo eee 8:3
Height of are of posterior and outer lateral
GUIET® (GD. 70) elotame ieee atch eon ee 2°3
Length of chord of posterior convex margin
(10s BAD) 36 ous bthio aan a Geass ee ean eo
Height of arc of posterior convex er
(ib: 0). 33
Thickness of median ridge where broken | in
middle of its course (left coracoid)...... 0°91
Thickness of anterior region of coracoid.... 0°25
Thickness of posterior region of coracoid .. 0°6
A60 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
The Scapula.
This (fig. 5) consists of a ventral plate, from the outer lateral margin
of which a lateral plate arises and ascends towards the dorsal surface,
its plane being inclined to that of the ventral plate at an angle of
about 90°. The ventral plate is longer than broad, thicker behind
than in front, truncated by a slightly convex edge anteriorly,
bounded by a widely open V-shaped margin’ behind, the inner stroke
(cr) of the “ V ” representing its articulation with the coracoid, the
outer stroke (v p)its share in the glenoid cavity tor the humerus. The
Fig. 5.—Diagram of Right Scapula. (Drawn reversed, scale 3.)
inner lateral margin is concave, the outer straight ; and from along its
whole length the lateral plate arises. The latter is like a long sca-
lene triangle in shape, the apex iying in front, the longest side being
that common to it and the ventral plate, and the next longest its
outer edge ; the base of the triangle is not a straight line, but a deep
concave curve arising from the anterior edge of the glenoid cavity,
passing forwards and upwards and then backwards to the end of the
outer edge. The lateral plate, when complete, is not bounded by a
simple outer or upper margin, as here described, but is prolonged
upwards along its posterior third into a thin narrow ascending pro-
cess: this process is broken off both scapule in our specimen; and
the posterior third of the outer edge of the lateral plate is conse-
quently a surface of fracture.
Dimensions of the Scapula.
inches
Length of outer edge of ventral plate (fig. 5,ap) ........ 81
Breadth at distal end (ib. ab) ............. Perr... 2:4
Length of chord of concave inner margin (ib. 6c) ........ 5:05
Height of arc of concave inner margin (ib. d) .......... 1:2
Length of articular surface for coracoid (ib.cr).......... 22
Length of articular surface for humerus (ib. 7p) ........ E93
Length of chord of posterior concavity of ascending plate
Gbl mm) Rien: 2-1
Height of arc of ‘posterior concavity of ‘ascending plate
FROM THE LOWER LIAS OF CHARMOUTH. 461
Restoration of the Pectoral Girdle. (Plate XXIII. fig. 3.)
The displaced bones retain their original outline so perfectly, that
if it were possible to move them relatively to each other into their
original positions the pectoral girdle would be well restored; as,
however, the stony matrix in which they are imbedded renders this
impossible, [ have made careful outline drawings of the several
bones, and then cut these out and fitted them together, being guided
in doing so by a direct study of the bones themselves. The result
is given in the diagram (Plate XXIII. fig. 3).
The furculum lies in front in the middle line; and the prescapular
processes of the scapule abut each on its own side upon the outer
posterior border of the furcular body proper, covering its wings,
which appear to lie in the angle between the ascending scapula and
its prescapular process. The lapels face the anterior projecting
convexities of the co1acoids without touching them. There is thus
produced a single continuous foramen, bounded laterally by the
concave inner borders of the scapule, anteriorly by the furcular
lapels, and posteriorly by the anterior margin of the coracoids; it is
wide from side to side, narrow from before backwards, and roughly
resembles in form two brackets joined face to face, thus :—@—
In the fact that the foramen is not subdivided into two by the
overlapping of the furcular lapels by the coracoids, this species differs
from some other species of Plesiosaurs; a corresponding difference
is displayed in the pelvic arch, the foramen between the pubes and
ischia, likewise double-bracket-shaped, being continuous from side
to side, and not divided into two, as happens in most other Plesio-
saurs.
The Humerus.
The right humerus is carried over to the left side, and lies with
its flat posterior surface uppermost (Pl. XXIII. fig. 1), For the proxi-
mal third of its length it is a thick cylindrical bone, with an ellip-
tical transverse section, the major axis being twice the length of the
minor axis (4 inches and 2 inches respectively); it then widens out
into a broad plate-like distal portion for the remaining two thirds of
its length. The ulnar margin is almost straight, only slightly convex;
the radial more curved and concave. It is covered superficially
with irregular longitudinal ridges, more abundant on the radial than
the ulnar side, which is almost smooth, and most marked near the
ends of the bone; at the anterior end they become broken up into
irregular tubercles.
The left humerus is similar to the right; but its surface is
smoother, and its proximal half less elliptical or more circular in
section; it begins to widen a little past the middle of its length,
widens and flattens then rapidly, becoming very thin (7 inch)
towards its distal edge. The more rapid expansion of the left than
of the right humerus is almost certainly due to compression, though
without the latter bone for comparison we should have nothing to
462 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
indicate this; hence a possibility to be borne in mind in making
specific determinations of isolated bones.
The Radius.
The right radius is a straight, almost parallel-sided bone, elliptical
in transverse section, truncated by slightly convex ends; it has a
simpler outline than is usual in Plesiosaurs. The left radius, which
has suffered more from compression, has more of the usual Plesio-
saurian outlines: its outer edge is gently concave, its ulnar margin
tricurvate, the middle curve being concave inwards; and its once
cartilaginous articular surfaces have been squeezed beyond the edge
of the flat surface of the bone. It is much ridged longitudinally,
the ridges diverging a little from the middle towards the ends.
Representing the length of the humerus by 100, that of the radius
will be 37; and this number may be called the humero-radial index.
Its value for other species is found in the table on page 477. For
P. rostratus it will be seen to be almost the same as for P. Cony-
bearer.
Dimensions of Humeri, Radi, Ulne, and Femora.
| Diameter of | Diameter at Diameter of Length
| head. middle of length. distal end.
[Saye ca from capi-
Ra. (Ol ANG IP Wen, WAL wy TP. Ra. Ul. A. P. | end to end.' tular ridge
_—— to end.
Humerus :— chord.| are.
Right...... 35 | 2:9 39 2°0 6:7 S21 1-22) ass | 15 A.
14-25 P.
Mhefti i teoe (?)36 | 3:2 39 2°0 nea BD) | oa 14:8 14°8 P.
Right...... 35 1 3:6) 84) 0 2:0) 67 0s we alee 1425 | 12-75 M.
13°5 A.
ett s 35 | 38 37 16 ace aap allege 14:37 13°37
Right...... eas aus SO os 35 375 | 0-7 5°45 ne
ett: eee. 39 | 08 315 | 055 | 3:5 3°5 | 0:55 5:0 4°75
Right...... ARESy Wo 39 ae 4°85 | 65 | O7 55
MHGLt vate) 2.8 | OF 37 re 4-7 6:0 56
Ra. Ul. means from radial to ulnar margin; A. P. means from anterior to
posterior margin ; Chord means measured along chord of curve; Arc means
measured along curve itself. In the last column A., M., P. mean measured to
anterior, median, and posterior edge of distal margin respectively.
The Ulna.
The right ulna, like the right radius, retains more of its original
form than the corresponding bone on the left ; for although its distal
two thirds are much flattened, its proximal third still presents its
original thickness.
This uncompressed portion has a smoother surface than the other,
FROM THE LOWER LIAS OF CHARMOUTH. 463
which is distinctly ridged; the entirely compressed left ulna is
ridged all over ; and this leads one to suggest that the ridges on fossil
bones may in some cases have been subsequently produced by me-
chanical pressure. Let the soft cancellous interior of a bone be
crushed together, and the denser outer layers, in adapting them-
selves to a more circumscribed area under pressure, may possibly
become finely wrinkled, and thus give rise to a spurious appearance
of ridges.
The Carpus.
The carpus, 7°25 inches in breadth, consists of two rows cf three
bones each, which diminish in size from the ulnare to the radiale.
They are polygonal bones, with the dimensions given in the table
below. In the left manus the distal row of carpal bones alone
bears the fingers, the radiale carrying one, the intermedium and
ulnare two each. In the right manus the ulnare of the proximal
row appears to bear one finger, the ulnare of the distal row two,
the distal intermedium one (but it contributes a small facet for the
adjoining digit of the ulnare), and the distal radiale, as in the left
manus, one.
Length. Breadth.
;
Radial. Inter- Ulnare. || Radial. | Inter- Ulnare.
medium. | medium.
Proximal series... 16 J3 2°65 215 | 25 2°75
Distal series ...... 1:8 14 2:9 2 Pale ice | 2a
The Manus.
The hand, where broadest, is 8-5 inches across. It consists of five
digits ; the first, with five phalanges, is incomplete in both hands; the
rest are complete in the left manus—the second, third, and fourth
having nine, and the fifth eight phalanges. The third and fourth
fingers are the longest. The phalanges have the usual form, a
compressed hour-glass outline,—except the most distal, which is
triangular, and apparently equivalent to the proximal half of one
of the other phalanges, the distal half being suppressed: it has
much the appearance of an ungual phalanx, and may very well
have borne a nail.
The measurements of the phalanges are averages of those of the
right and left manus, and in the case of the breadth, of the distal
and proximal ends of each phalanx.
464 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
Phalanges.
Length. Breadth.
Tih ta aoa ave {. 1 s/s er ane ave Vv.
Tee tap 19 25 30 30 31 1:25 115 1:35 1:35 75
BIS dered 18 23:5. 25 26 2:45 weet 1:85) cA 2 oie
DID ics: SO MEDI AIP Seeks. Diva 12) 4b 1-4 ae eles
LVR asthe oe 18 1°75 1:95 1:95 2:0 i ce, 1:25) L2o eo
See id 1°75 2:05 1.7 1:65 1:66 PYb oo fi5: 131 O95 aes
Wilson cnt 18S hei) leek hn4) a 9 10 O08 O07
Video a esate Pa ESSs be) ee oils) 0:72; 072 107 tas
VAUD Se cies 10 O8 1:0 0-45 055 045 0-45 0:35
ch Coates 08 O7 O68. 044 03 03
Total length a ? 17 18 18:25 16:8
fingers ......
The Pelvis.
A restoration of the pelvic girdle, obtained in the same way as
that of the pectoral arch, is given on Pl. XXIII. fig. 4.
The Pubes (fig. 6).
These are more or less quadrangular plates, which meet each other
in a straight median symphysis along nearly their whole length.
The anterior margin is an undulating curve, with a general direction
at right angles to the symphysial margin. The posterior margin, at
first a little convex, becomes concave for half its length outwards
from the symphysis, then almost straight and parallel to the ante-
Fig. 6.—Diagram of the Right Pubis and Ischium. (Scale 3.)
_Ylor margin as it articulates with the ischium; finally it curves
forwards and outwards, to contribute its share to the acetabulum,
and joins the outer margin, which has a slope obliquely outwards as
it passes backwards from the anterior margin.
FROM THE LOWER LIAS OF CHARMOUTH. 465
The Ischium (fig. 6).
This “ shoulder-of-mutton ” shaped bone meets its fellow for about
half its length in the median symphysis. The m-shaped anterior
margins of the two ischia meet to form together a bracket-like out-
line (——~) ; the similarly shaped posterior margins of the pubes
do the same; and the brackets facing each other give rise to a
foramen, which is continuous from the pubic ischial smyphysis on
one side to that on the other. In this character the pelvis resembles
that of Murcnosaurus, Seeley, Q. J. G. S. vol. xxx. p. 206.
The Ilium (fig. 7).
The ilium has the usual Plesiosaurian form, a central shaft with
expanded ends, compressed in different planes, which are inclined at
about a right angle with each other.
Fig. 7.—Diagram of Right Ilium. (Scale 3.)
d
P
=
Measurements of Pelvic Bones.
Pubis. anne
Womepieaisy lap ltysis (112. 6,09) ) Sicsasss os coc sce vonn sc scseccweesencc rues sas 5°5
Breadth of bone from symphysis, and along a line at right angles to
it, to anterior edge of acetabulum (ib. fl) ..........2...s.ceceeeeer eee ee
Maximum antero-posterior diameter, drawn from d! .................. 81
Length of diagonal from inner anterior angle to anterior edge of
eice allo whtinie (AONE ae. oc Ania clas ene Ret acetates 10°3
¥ from inner anterior angle to posterior edge of
its share of acetabulum (@ 0) .................+..- 10:3
3 “5 from outer antero-posterior to inner posterior
EPELO (Lp) Meee fess 5, § Lavage Rai eases 9-0
iy articular surface for acetabulum (f 0) .................0.s006 2°9
a te Wn a {OIE TEG ATTN (DG) mesa seeaeossockosaceeseeenees 2°3
a Chord Om posterior concavilby|(GIN)2 5,-2.0... eee ses eaetcass 39.
Height of are a pk) RS ESR ee RRR a eae eS 2 1:25
Ischium.
Mienethohsympbysis (a p!, fig. G):..102:.-0.0.82.s0250002-cageceseep esses 5'5 to 6:0
Breadth along a line at right angles to symphysis to posterior edge
ni sapetnloml en (GD) ese owe nec eee aren AnE eR PPE Dose uaeaepcoddccore cou
Length from outer edge of its articulation with the pubis to its pos-
PeRAOIEAIS Loy (OM) kita Noses cerca eeeea toon seen adicc Soe ebatiies sane neces 10.1
Length from anterior inner angle to posterior angle (N D)............ 7725
Minima diameter across ‘neck 7 (72 &) , ~.....02-02sssecenssurmseeeacenee 2°4
Length of symphysial margin for pubis (0 €) ................0 cee eseee eens 2°4
ts Tee copula aneine (Oye ee te. aoc acincoveaemaceee acest ae 25
. chord or anterior concavity (GIN) 5....2--s.a.cessoneseeeee sees 3°85
ein onarc of anterior concavity (@) ..2....2-22-:0ssessscateecaeeeesson= 18
466 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
Ilium.
Right ilium. Left ilium.
inches. inches.
Mrenabla (07; O17) sos. we atecles idosin cite nyecednee Serene eae 6-9 72
breadth of proximal end)(pp) \o 22... 224 scee= sees see 2°4 (2) 2°85
3 distal (@'d)B3s eo ese e eee 2°3 1°9
Minimum diameter of shaft (77 772)................0000 ae 1:0
Note.—The proximal end of the right ilium is slightly broken, and its distal
end compressed, probably by subsequent pressure.
The Femora.
These bones, which are smaller than the humeri, have the arti-
cular head well defined by a sharp surrounding ridge; the articular
surface itself is deeply pitted and tuberous, indicating the previous
existence of a thick covering of cartilage which has since dis-
appeared.
The cylindrical proximal end is slightly constricted below the
capitular ridge before it begins to expand. ‘The dorsal and ven-
tral margins are almost straight lines, or only slightly concave
curves, which diverge gently from the thick proximal to the broad
and flattened distal end. ‘he distal end is truncated by a simple
gently convex curve.
The surface of the bone is roughened beneath the head, and
strongly ridged at the distal end with-longitudinal lines, which
diverge in conformity with the curves of the lateral margins of
the bone.
The Integuments.
Remains of what appears to be some dermal structure have been
stated by previous writers to occur in connexion with Ichthyosaurus ;
and Charles Moore in particular has well described a thin layer
having a wrinkled surface, which invests a large number of the
Ichthyosaurs in the collection of the Bath Museum; but no one, so
far as I know, has made mention of any similar investment in the
case of Plesiosaurus. Great interest therefore attaches to the
presence of a thin brownish film, with characteristic surface-mark-
ings, which coats a considerable portion of the specimen under con-
sideration.
It is best displayed on the surface between the fortieth and
sixtieth vertebrae, covering the bodies, transverse processes, and
neural spines of the vertebra, the ribs, and the surface of stony
matrix intervening between them. It also extends in a band over
an inch broad, along the distal ends of the neural spines, at a little
distance from them as now exposed.
This band, which seems to restore the dorsal outline, ends in the
pelvic region, where it covers the head of the right femur, and
imbeds a small oblong bone, the smooth shining surface of which
is raised into three parallel longitudinal ridges ; other fragments of
FROM THE LOWER LIAS OF CHARMOUTH. 467
similar bone are indicated near the same spot. Their presence can
scarcely be accidental; and they may possibly be dermal plates.
That they are not found elsewhere would simply point to the
restricted distribution of dermal scutes in the species, they having
originally been present in the pelvic region and nowhere else.
The thin film, however, has nothing of the nature of scales and
scutes, so far as we can see; it was a continuous membrane, not a
collection of separate individual structures. It can easily be
detached from the underlying surface, owing, it would seem, to the
presence of a thin whitish layer, apparently calcite, which is more
strongly adherent to the film than to the surface beneath.
The surface of this film is variously marked ; but all the different
markings may be described as essentially of the nature of
wrinkles. In the film of the dorsal band they have the appear-
ance of fine regular rounded ridges, giving the surface a re-
semblance in some degree to “ corded silk;” elsewhere, as over the
bases of some of the neural spines, the ridges lose to a great
extent their straightness and regularity, take a tortuous course,
though generally with one prevailing direction, and are more appa-
rently mere wrinkles; but over the greater part of its extent an
additional feature presents itself in the form of long, fine, parallel
grooves, bordered by fine ridge-like margins, and looking as though
they had been scored by a fine needle: they vary in distance from
each other; but the best-marked are about 4, inch apart. They main-
tain one general direction from before backwards on the bodies of
the vertebree, the exposed outer sides of the ribs, and on the stone
between them, from the forty-second to the fiftieth vertebra.
Between the grooves minute wrinkles are abundant, mostly undu-
lating, sometimes straight, not always confined to the space between
two grooves, but sometimes crossing them without changing their
course; they are inclined at all angles to the grooves, but are
chiefly transverse to them.
What the precise nature of this film may be is by no means
clear. From its distribution one might infer that it originally
formed a part of the integumentary investment. It closely resem-
bles in character the structure which has been regarded by Mr.
Moore as forming a part of the integument of Ichthyosawrus, and
which this acute observer has compared to the wrinkled surface of
the skin of the Porpoise*. The resemblance between this surface,
as seen in our museum-specimens, and that of the investing film
in Plesiosaurus is, indeed, great; and if such a skin were capable of
fossilization, one might fairly allow that Plesiosawrus had been
invested with it. It is very certain that the film in our fossil
specimen was of a yielding flexible nature, or it could not have so
neatly covered the exterior of the ribs and adapted itself to the
ends of the transverse processes and the angles between the neural
spines and the vertebral bodies as it has done.
* Som. Archzol. & Nat. Hist. Soc. Proc. 186-566, p. 179.
468 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
Classification.
The pectoral arch in its essential characters is truly Plesiosaurian,
though it differs from most Plesiosaurs in the fact, if it be a fact,
that the coracoids do not extend in front so as to overlap the
“lapels ” of the furculum.
To make plain its relations to other members of the genus Plesio-
saurus, I have constructed the following Table, in the last four
columns of which the distribution of the vertebrae amongst the
various regions of the spine is given for each species.
In comparing the length of the head with that of the neck (or
rather of the cervical series of vertebra) I have uniformly made use
of the proportion :—
length of heaqg_ I
length of neck 100°
The value found for I may be conveniently called the cervico-
cephalic index. This index is given, for each species in which it has
been determined, in the first column of the Table.
In the second column I have similarly compared the length of
the head and the dorsal series of vertebree (excluding sacral vertebree).
The indices of this column are dorso-cephalic.
The total length has not been made use of in comparison, since it
is seldom possible certainly to obtain it, and variations in the length
of the caudal region are of secondary value; but in the third column
values are given for the length of the head compared with the cer-
vico-dorsal series (exclusive of sacral vertebre). ‘To the cervico-
dorsal cephalic index great value may be attached, since it can
frequently be obtained and is independent of any error in the method
or the practice of determining the position of the last cervical ver-
tebra. It is true it may be affected by a mistaken determination of
the first sacral vertebra; the sacral vertebrae, however, are more
easily determined than the last cervical; and an error with regard
to them will not cause a deficiency or excess of more than one or
two vertebre to the cervico-dorsal series, while I am convinced
much larger errors have been made with reference to the number
of vertebree in the cervical series ; and, finally, in comparatively so
great a length as that of the cervico-dorsal series one or two vertebree
more or less will have but a trifling effect on the value of the index
obtained fromthem. Another index of some interest is the cervico-
dorsal, obtained by referring the length of the neck to that of the
trunk taken as 100,
The values now given for the various indices will certainly in
many cases need revision, since the measurements on which they
are founded are often extremely unsatisfactory. Sometimes they are
unreliable or erroneous, sometimes vague (as when the length of the
‘“‘trunk” is given without stating whether the sacral vertebrae are
included or not, or when the length of one part is given in fractions
FROM THE LOWER LIAS OF CHARMOUTH. 469
of another*; and sometimes, finally, they are not comparable, as
when in one place the length of the skull is given (as it too frequently
is) as the length of the lower jaw, while in another it is taken as
the length between the end of the snout and the basioccipital.
On reference to the Table it will be seen that P. Conybeare has the
same number of cervical vertebree as P: homalospondylus, but one
less dorsal: its head, however, is much larger than that of the
latter species; and hence there is a great difference in their re-
spective cephalic indexes. In proportion of head to neck it agrees
exactly with P. Hiheridgu, but differs widely in the number of cer-
vical vertebre. It has also two dorsal vertebre fewer ; and its dorsal
and cervico-dorsal cephalic indexes are distinctly different. Its
cervico-dorsal index approaches nearest to that of P. Hawkins, nm
which species this index attains its maximum value.
; Cephalic indexes. Number of vertebree. Gadel odl ae ;
2 | - umero-
_ Plesiosaurus. a x oe dorsal | racial
i O- Tso- in ° ina@ex
ceuhalte. éeotalie. ome Cerv. | Dors. | Sac. Cau. ox
ters 876 58°3 33°9 at Mee ae a 722
BEGAGTIS....0c.c000. 63:9 Eyles 28:4 24 24 2 34 is SY a
ropinguus ...... 60:0 Hore 28°85 |} 25 23 2 34. 92°6| 45°8
Dramptoni......... 55-5 416 24:0 27 30 2 32 750| 28°5
megacephalus 53°3 | 493 | 26°5 30 26 2 34 92:6; 33:5
macrocephalus ...| 51:2 65°6 28°8 29 20 2 1280} = oO
brachycephalus...| 35:3 | 403 | 188 31 24 2 21 | 1140; 333
Ongirostris ...... 338 29-7 158 33 25 32 (2 We SS
Hawkinsii ......... 30°0 46:9 18:3 31 23 2 TaG2 fo4s7
Etheridgii ......... 24°3 26:0 125 30 23 2 34 106:0
ponybeari ......... 24:1 37°4 14:6 38 21 2 5+) 153:0| 37:0
lolichodeirus...... eT 23°6 10-1 4] 21 2 380+] 133°3|) 42:9
macropterus ...... 12°8 17:0 UD 39 24 1? 28 1320} 50:0
homalospondylus} 106 | 11:1 o4 38 22 2 105°0| 46-0
There is a fine specimen of Plestosaurus in the British Museum,
with the MS. name P. laticeps, Owen, which bears a close resem-
blance to P. Conybeari. Its pectoral and pelvic girdles are well ex-
posed on their ventral surface, and are strikingly similar in general
form and arrangement to those parts in P. Conybeari; the dimensions
of their component bones also show a general agreement, as will be
seen from the following table. In each the humerus is longer than
the femur; but these bones are each an inch shorter in P. laticeps
than in P. Conybeari.
* Thus, in his Monograph on Liassic Reptiles, Professor Owen says of
P. rostratus that the skull is # the length of the neck. Now the skullis 1 foot 11
inches long; and thus the length of the neck should be 2 feet 6 inches 8 lines.
But he also says that the length of the neck is rather less than 4 the length of the
spinal column; as the latter is 9 feet 9 inches long, the neck should be “‘rather less”
than 3 feet 3 inches long. Whereabouts between these two quantities is the
exact length? And would it not seem to have been easier to direcily state it?
Unfortunately the instance here given does not stand alone.
Q.J.G.8. No. 147. 21
470 PROF. W. J. SOLLAS ON A NEW SPECIES OF PLESIOSAURUS
Table of Measurements of corresponding Parts in P. laticeps, Owen,
M.S., and P. Conybeari.
P. laticeps. P, Conybeari.
inches, inches
Puneuluu’ leneth (aspscias) cesses steers eee sees 60 6-4
@oracoid) tength (Gnaximiura) i ee5 ees eee eee 17-0 17-375
is breadth: siajohiadscstenmecen. a costee merce eeee 80 8:0
Pubis, length of symphysial margin (a.p. dia.) ......... 6°5 55
< » parallel to outer margin (a.p. dia.) ...... 8:0 81
is, » Oblique diameter from inner anterior to
postero-exterion angles way see cee ase ee eee nee eee eee 10:0 90°
Ischium, length |(@max.voblidias)im---sse- eee casera 9-0 10-1
Humierus, length. £iirccsas. bec ecdoce cee cena nce ce eee 13°5 14:5
Hémur; length: sa2.e. sae. tarenteate es cota eenece ee emcee 12:5 13°5
Neck, from first cervical vertebra to anterior edge of
furculumes..Uiten accaee sere. sane ee eee oem 56-0 780
Trunk, from anterior edge of furculum to posterior
edgesor pubis’ ast-ccusnnetecese eee cece rere 48:0 53°90
Number of cervical vertebre from first to anterior edge
Of furculumy Sincere casos et aaesas rae eee eres 27 38
ength of posterior cervical vertebra ne-eea-eeeeeeeeeee 2°25 25
Lengthrot dorselivertebra i. s-ss eee ee eee eee 2'375 2°65
The anterior end of the head is brcken off and missing in P. lati-
ceps ; so that the cephalic indexes cannot be determined.
The regions of its vertebral column cannot be clearly defined,
since the pectoral and pelvic girdles conceal to some extent the ver-
tebree beneath them. There is no great difference in the length of
the dorsal region of the two species ; as shown in the Table, in P.
Conybeari it is 5 inches longer than in P. latieeps, a difference which
may be accounted for by supposing the furcula of the former to be
displaced a little forwards.
The widest departure is seen in the neck, its length being much
less and the number of its vertebree much fewer in P. laticeps; but
there is an artificial look about the neck of this specimen which leads
me to conjecture that some of the cervical vertebrae may be missing,
so that, if those which remain were arranged as they were first
found, several considerable lacunz would appear between them.
The lengths of the centra of the cervical and dorsal vertebree
make a close approximation in the two species, P. daticeps in this, as
in several other characters being a little the smaller. The anterior
cervical vertebra of P. laticeps are rugose or tubercular in the same
fashion as those of P. Conybeari.
Finally, both species come from the same “ gisement,” the Lower
Lias of Charmouth.
If my conjecture with regard to the identity of the two species
should prove correct (and it will require a closer examination of
Owen’s species than I have been able to give it to decide this), then
of course the name “ latzceps ” will have to be suppressed. It occurs
in print in the ‘Geological Magazine,’ vol. iv. p. 144, but without
accompanying diagnosis or specific description.
One other character of P. Conybeari alone remains for comparison ;
and that is the relative dimensions of its vertebral centra. If we
find the proportion of the breadth and height of a centrum to its
FROM THE LOWER LIAS OF CHARMOUTH. 471
length taken as 100, we shall obtain its latitudinal and altitudinal
indices. These are given in the following Table for the cervical
yertebree of a number of species. To make their comparison of
yalue, corresponding vertebre should be selected for each species ;
and for this tables like that on p. 452 would have to be constructed
and discussed. As it is, I have had to make the best use I could of
the material ready to hand in published papers, and to trust to the
chance of different describers having given measurements of an
average cervical vertebra. Most of the indices in the table have
been derived from the thirteenth to the fifteenth vertebra, and
probably are sufficiently comparable.
Plesiosaurus Hea ees Number of vertebra.
Wonywedey - 20.2. .62-.-5-- 70 100 XV.
homalospondylus ......... 92 72 XIII & XIv.
SUP USS apace ene 107 100
ecelospondylus ............ 110 106 XV,
(TIGRIS Caicos anceaeee enone 112 84 XV.
BRP ACEOUNGUS soc occ edecccces 112 100 Middle.
: Average of middle and
infraplanus .............4. 113 101 ve a Pee ee
dolichodeirus............... 113 94
PRCWADIISTO cose cc access ese 116 116
Sather 120 98
SLOUL PAUSE ..2...:- +++ 123 115
a WGINGID oc ch-os-c0000--5- 125 112
TeLICING. ache seee eee 127 102
Glenutheraxonm ............25. 127 100
CORR 134 119
SUDEFIZONUS | ...5....5.-004- 140 109
GMOMPCTISNS .c20-- cts cciceccnse 140 116
BACIVONAUS. 2.50.20 5000000 0: 42 110
SULOCUIN Scenes 150 120
eleutheraxon ............... 169 100
Li 170 155 XV.
It will be seen that the centrum of the fifteenth vertebra of P.
Conybeari has a lower latitudinal index than any other known spe-
cies, while its height remains about the average.
P. homalospondyius, which makes the nearest approach to it, is
equally remarkable for its exceptionally low altitudinal index.
The compression which the cervical vertebrae of P. Conybear have
undergone may to some extent account for the narrowness of their
centra; but it cannot be altogether explained in this way, since it
persists in a marked manner down to the twenty-eighth vertebra.
Moreover our measurements were taken from the articular ends of
the centra; and these show no obvious signs of compression.
The Table shows a general tendency in the long-necked species
towards a low latitudinal index, and in short-necked species towards
a high one; but the rule is subject to exceptions, and we have not
enough instances to reason from. The latitudinal has clearly a
greater range of variation than the altitudinal index.
212
AT2 PROF. W. J. SOLLAS ON PLESIOIAURUS
Notes on Plesiosaurus megacephalus, Stutchbury, and
P. brachycephalus, Owen.
The type specimens of these two species are preserved in the
Bristol Museum ; so that I have had a good opportunity of making
a close acquaintance with them, and have succeeded in elucidating
some points in their anatomy which were hitherto obscure.
PLESIOSAURUS MEGACEPHALUS.
1. The Roof of the Mouth.—The skull of this specimen lies on its
dorsal surface, separated from its matrix from the snout to a trans-
verse fracture which traverses it across the orbits. The matrix
has been carefully chiselled away from between the rami of the
lower jaw, so as to clearly expose the roof of the mouth and the
base of the skull for its entire length. The anterior part of the.
base (fig. 8), which lies in front of the fracture before mentioned, is
by a most lucky chance much better-preserved than that behind, and
thus affords us an opportunity which has long been desired of ascer-
taining more exactly the true nature of this part of the skull.
Fig. 8.— Ventral View of the anterior Part of the Skull of
| P. megacephalus. (Scale 3.)
2, internal naris; f, palatal foramen.
It presents, about 2 inches behind the end of the mandibular
symphysis, two oval foramina (fig. 8, 7) longer than broad (1°45 inch
in length) separated from each other by a bone which extends back-
MEGACEPHALUS AND P. BRACHYCEPHALUS, 473
wards in the middle line and unites by a splintery suture with the
palatines behind. Itshows traces of a straight sutural union along its
median antero-posterior diameter, and consists, without doubt, of the
connate vomers. On their outer margin the foramina are bounded
(fig. 9) for the anterior three quarters of their extent by the maxille,
for the remaining quarter and along their posterior margin by the
palatines, and along the inner border (as before mentioned) by the
concave outer margin of the conjoined yomers. The vomero-palatine
Fig. 9.—Diagram showing the left Internal Naris of P. megacephalus,
bounded by the Maxilla, Vomers, and Palatine. (Scale 3.)
Vo a P I}
suture has more or less the shape of a W, as exposed on the floor
of the skull, the apex of the W being on the median line, and
the end of its lateral strokes cutting the inner posterior angles of the
foramina.
The palatines extend backwards for some distance as flat, hori-
zontal plates, suturally united in the middle line, and completely
roofing over the front of the mouth. Their sutural union is inter-
rupted for a part of its course by an elongated vacant space (fig. 8, f)
which clearly corresponds to the palatal foramen of many Lizards
(e. g. Iguana, in which it is well seen).
An oblique linear fissure starting from the middle of the outer
stroke of the W of the vomero-palatine suture runs on each side out-
wards and backwards, to disappear against the matrix bounding the
roof of the mouth. These fissures might easily be mistaken for
sutures, in which case they would be regarded as indicating the line of
junction of the palatines; they are, however, simply fractures
which have broken the palatines along a line where they become
flanged upwards and outwards to join the maxilla. The fractures
are, indeed, continued through the skull; so that the middle part of
it, included between them, can be readily separated from the outer
part on each side, and the form of the palatines and their union _
with the maxille clearly exposed (fig. 10).
Another fracture traverses the skull nearly vertically, but oblique
to the axis, passing through one of the external nares, and one of the
oval foramina, or nares, as we may venture to call them, before
mentioned. This fracture shows (fig. 11) a large central chamber,
now filled with the Lias limestone; it is bounded above by the
474 PROF. W. J. SOLLAS ON PLESIOSAURUS
Fig. 10.—Oblique Fracture through the Skull of P. megacephalus,
showing the line of union of the maxilla and palatine. (Scale 3.)
In, Internai nasal passage.
premaxille, below by the vomers and palatines, and on each side by
the maxille, and also in some parts of its course by the palatines.
Fig. 11.—Transverse Fracture through the Skull of P. megacephalus,
crossing the nasal chambers. (Scale 3.)
tK[ppyo
yyy
SLLLLINCL
EN, external naris; JN, internal naris.
The vomers (fig. 11, Vo) form a trough-shaped bone of considerable
thickness, flat below but concave above, with a low ridge on each side
of the middle line ; its sides extend upwards, together with a process
from the palatines, as a curved wall for half the height of the central
chamber, which is thus divided through its lower half into a middle
and two lateral portions. ‘The lateral portions have the appearance
of tubes sloping downwards and forwards. On each side of the
premaxille the external nares open freely into the central chamber ;
while the foramina on each side of the vomers communicate with its
lateral passages. These passages are bounded externally by the
maxille, and internally, as well as inferiorly, by the palatines.
The oval foramina appear to represent the internal nares, since
they are similarly situated with respect to the surrounding bones as
the posterior nares of many Lacertilia ; and it is with this order that
Plesiosaurus stands in the closest connexion.
MEGACEPHALUS AND P. BRACHYCEPHALUS. 475
It must be borne in mind, however, though I doubt whether it is
generally known, that the posterior nares by no means occupy
a constant position in the Lacertilia; for though they are most
usually bounded in the manner above stated, they sometimes shift
their position backwards and open at the back of the palatines. In
such cases, however, the palatines are produced towards the middle
line, each aleng its cuter edge, into an underlying plate, which roofs
ever the mouth and forms a floor to the nasal passages. A section
across the Plesiosaurian skull might be expected, therefore, to give
some signs of an inflection of the palatine bones, converting them
into incomplete tubes, if such a backward extension of the nasal
passage obtained init. No such signs, however, are to be detected
in the specimens under consideration. A diagrammatic sketch of a
fracture passing transversely through is given below (fig. 12); it
shows plainly the outward and upward bend of the palatines, but
not a trace of an infolding.
Fig. 12.—Transverse Section across the Skull of P. megacephalus,
showing the palatal plates flanged upwards and outwards towards
the Maxille, but not inflected to form a nasal passage.
e)
' O a
a eee
It is a fact too curious to be passed over, however, that the
internal are situated in advance of the external nares of this
Plesiosaur, the anterior margin of the latter being a trifle under
2°8 inches behind that of the former.
A transverse section through the upper and lower jaws is given
in fig. 13: the upward flange of the palatine is seen meeting the
maxilla; and the lower jaw has the usual reptilian composition.
2. Redetermination of the Number and Distribution of the Ver-
tebre and of the Length of the Regions of the Spinal Column.—Of
cervical vertebre, twenty-nine are visible up to the anterior edge
of the furculum; in all probability one more lies beneath this
bone; and the total number may therefore be taken as thirty.
In consequence of the concealment of a large part of the spine
beneath the pectoral and pelvic girdles, the number of dorsal
476 PROF. W. J. SOLLAS ON PLESIOSAURUS
Fig. 13.—Transverse Section through the Jaws of P. megacephalus.
(Scale 2.)
Ans
T, tooth.
vertebre can only be indirectly arrived at. The total length of
that part of the vertebral column which lies between the anterior
edge of the furculum and the posterior edge of the ischium is
70 inches; from this 2°3 inches must be deducted on account
of the concealed last cervical vertebra, and 6-9 inches for three post-
dorsal vertebree supposed to be concealed beneath the ischium, two
of them being sacral and one the first caudal. This leaves 60-8
inches (70—2°3—6:9=60°8), which is the length of the dorsal
region. Divided by 2°3, the average length of a dorsal vertebra, this
gives 26°43, or, neglecting the fraction, 26, which is the number
of vertebre in the dorsal series. These numbers are embodied
in the annexed Table (page 477), in which the measurements of a
number of specimens of different species are compared together.
PLESIOSAURUS BRACHYCEPHALUS, Owen. (Plate XXIV. fig. 2.)
This species has not been figured, and has been only partly described.
I do not intend here to do more than offer a few observations upon it,
and to correct the previously made measurements.
1. The Skull.—Although incomplete and broken, the skull is but
slightly distorted, and presents several points of interest.
The snout is broken away from the rest of the skull, and shows
the under surface perfectly. It is 5 inches long, and does not
exhibit the internal nares ; so that they must have been situated
further back. Its broken surface extends at right angles to its long
477
MEGACEPHALUS AND P. BRACHYCEPHALUS.
. Total Sa- -, | Fore | Hind | Hu- | Fe- | Ra- 1 Ma-
Species. length. Head. | Neck. |Trunk.| am. | Tl. | imp. | limb. |merus.| mur. | dius. | 1b! | Ulna- Fibula ois. | Pes:
*megacephalus ...............| 195 | 30 56:3 | 60°83 | 46 | 54:5 | 33+ | ...... | 137 | 135 | 46 | 45 | 43 4'5
“© (Ovpsyaay ONAN Sec oodonsaneORoHOK 268 | 40 72 965 — J) eamecnd 66 GOD A misc 21 22 6 6° 6'5 6
tmacrocephalus .............| 59+] 105 | 20°5 | 16 15 | 11+ | 12.75} 18:5 4 Aaa) |) 12745) RE 1-16 |" Whe 8 9
tbrachycephalus ......... ...| 129 | 145 | 41 36 25 | 23 Sac ae | acoreeae poet OxGOnltenee sae IPAS) sonar. to)
IGM OIROSiMis enema cmenr iO meorrO le LOl 980) so dou (POO) 44 bay cal OC limanecnialfs 40 vehea iene
INGLE aehol-Ibh eoeeeeedeoneE ssocn, Wee (eon | 20 16 ee 20 Ome |aaliss Wate eo aerfoy oxo) fA) AD) te aS a accom | ee)
PAWPMEHOCWeneewaceee esc) 08) OO 128 26:5 | 2°5 | 26 pee ln wataenlic GROE at oh ALO
PIC OnV MCAT G cae. eveecvencs| Lik | 20 83 53'5 | 4:25) 10+ | 445 |...... | 148 | 14:25) 6°45) ..... DD) Geen oO
LOMICHOCOUOTISN cmevretstetteven|) wiles 85 | 48 36 Taoran: (od sepia See alee a 7 3 3 s-tgtetaehe| Meo eecenel pele 14
IMACKOPLELUS ...-crecree ses] LOa 9 70 53 escent RAO 42°5 | 46:5 | 12 11 6 5 Sheer leedeeee” 25
homalospondylus ........./198 | 9 |85 |81 |....../32 | 44 | 45 { ae her Pee lo) ag | avn 24
HOSHRENTUS | jogpoceooqoonouneene |f ets jp ae 1 Gls) 39 Fou, Oo 24 Pay 18) O7D | oo. | so Bide ses |e Le
FOO PUM CUUIS reece veins 180 30 | 50 54 ncosee | Or4 44 Teucey owe meteor leOlOs | teas ale WOO
ZELIENOIOUS savassceseeesccce 22S 4) | 52 72 Boies: |e stam hac ere ae
The measurements are given in inches.
In those marked * the length of the head is taken from the anterior edge of the premaxilla to the posterior edge of the quadrate ; marked
thus, t, it is taken as the length of the lower jaw ; thus, }, from anterior edge of the pramaxilla to end of parietal.
478 PROF. W. J. SOLLAS ON PLESIOSAURUS
axis, and since it has been polished reveals very clearly the arrange-
ment of the bones in this region of the skull (fig. 14).
Fig. 14.—Transverse Section through the Skull of P. brachycephaius.
(Seale 2.)
The upper and backwardly prolonged processes of the preemaxille
are seen on each side of the middle line above, the maxille bearing
teeth on each side, the vomers in the middle line below conjoined to
form a single trough-shaped bone ; a plate of bone forming the roof
of the mouth on each side of the vomers is an extension inwards of
the maxille.
The left orbit is complete and undistorted ; it is bounded by the |
usual bones, the sutures between them being exceptionally plainly
shown. An additional bone, which looks as though it had been
segmented off from the jugal, appears, however, between the jugal
and postorbital ; its surface is marked in the same way as the Jugal ;
and it bears a nutritive foramen, which completes the ascending
series of these openings carried by the jugal. The suture between
the two bones is distinct, however; and the striations on their
surface are so directed as to indicate their separate nature. If a
posterior supraorbital bone had worked its way in between the Jugal
and the postorbital, it would have the position here described; but
simulation of the appearance of the jugal bone wouid remain unex-
plained. Hence it seems best to call it a suprajugal.
The jugal and the suprajugal bones are not the simple bony plates
which they appear to be in a lateral view of the skull, and as the
jugal really is in recent Lacertilia. Both extend inwards behind the
orbit as a bony plate, which meets and joins externally with a
similar expansion of the parietal. In this way the orbit is com-
pletely walled in behind. The maxillasimilarly extends inwards in
front, no doubt accompanied by the lacrymal; and, below, a con-
tinuous floor is afforded by the expanded palatine. The orbit is
consequently very thoroughly walled round.
The right orbit is incomplete ; and a horizontal fracture enables us
to remove the jugal, the only outer boundary bone of it remaining,
from the floor of the skull below. The jugal thus removed is a
MEGACEPHALUS AND P. BRACHYCEPHALUS. 479
triradiate bone—when looked at from below, something like the
letter 7. ‘The crossbar of the T corresponds to the outer plate of
the jugal, the stem to the process which extends from it inwards.
The inner plate or process of the jugal does not join the outer bone
abruptly, but curves outwards on each side into it. Thus a trian-
gular space of considerable size is left at the junction of the two
parts, or, in other words, at the origin of the inner plate. This
space is occupied by coarsely cancellous bone, and lies immediately
under the nutritive foramina, which occur on the outside of the
proper jugal bone. The meaning of these foramina is thus made
clear.
The floor exposed by the removal of the jugal is very difficult
to interpret. Immediately behind the palatine is a narrow bone,
transverse to the axis of the skull, and apparently joining the
posterior edge of the palatine. Behind this, again, is a flat
parallel-sided bar or lath of bone, projecting from the middle of the
skull outwards at right angles to the axis; it 1s united by a splintery
suture with the inner margin of a large and important bone, which
extends backwards, prolonging the line of the maxilla towards the
quadrate. It consists of a vertical wall-sided outer plate, roughened
on the external surface (which is a flat plane), and an interior
horizontal plate, the inner angle formed by the divergence of the two
‘plates being neatly rounded into a concave curve. The inner margin
of the horizontal plate is a deeply concave curve.
The vertical plate of a bone having a similar position is shown in
the right side of the ventral surface of a skull numbered 14550 in
the British Museum. I do not know what to make of this bone; but
it appears to be that which Prof. Huxley has spoken of as quadrato-
jugal in his paper on P. Hitheridgu.
The posterior part of the skull of P. brachycephalus covers over
the axis and atlas vertebre. It consists of the parietal and the ends
of the two bones which have been called suprasquamosal. They
join in a splintery suture over the middle of the parietal, and appear
likewise to underlap it below ; so that this bone appears to proceed
from between the upper and lower tables of the suprasquamosal
bones. ‘This is a very singular feature; but as I have been able to
examine this posterior fragment of the skull on all sides, and partly
to take it to pieces, I entertain little doubt as to its existence.
2. Redeternunation of Measwrements.—Professor Owen says that
the vertebre, at least as far as the 28th, are cervical; but a careful
examination leads me to include the 29th as an indubitable cervical
vertebra. The succeeding vertebre have lost a slice from their
exposed sides; but there is good reason to conclude that the 30th
and 31st also belong to the neck. ‘The length of the cervical series
is, then, as follows :—
I and IT concealed+ III to XXIX undoubted cervicals+ XXX and XXXI doubtful.
1S5inch + 36 inches + 3°5 inches
=A] inches or 3 feet 5 inches.
480 PROF. W. J. SOLLAS ON PLESIOSAURUS
The remaining measurements are given in the appended Table
(p. 477).
meee Horizon.—Associated with this specimen, which came
from the Lias of Bitton, are some Ammonites and Rhynchonelle,
which Mr. Whidborne regards as A. Conybeart and R. variabilis ;
hence he refers it to the A.-Bucklandi zone.
In concluding this paper, I have to offer my best thanks to
Mr. Etheridge and Dr. Henry Woodward for the kind assistance
they have given me in many ways; to Mr. Whidborne I am espe-
cially indebted for much useful help, and particularly for his care
and assiduity in drawing up the appended list of species, with their
geological positions, many of which have been determined by his
own personal examination of the original types.
EXPLANATION OF PLATES XXIII. & XXIV.
Puate XXIII.
Plesiosaurus Conybeart.
Fig. 1. Ventral aspect of the skeleton. One twelfth nat. size.
2. Dorsal aspect, showing the vertebral column from the thirty-seventh
(xxxvi1) to the sixty-third (ux) vertebre. About one eleventh
nat. size.
3. Diagrammatic restoration of the pectoral girdle. One eighth nat. size.
4, Diagrammatic restoration of the pelvic girdle, the ilia not being repre-
sented. One eighth nat. size.
Pruate XXIV.
Fig. 1. Skull of P. Conybeari, left side. About one fourth nat. size.
2. Skeleton of P. brachycephalus, Owen. About one twelfth nat. size.
Discussion.
Prof. Srerzy said that without an inspection of the evidence
he was not in a position to criticise this elaborate paper; but it
gave evidence of painstaking research of no ordinary kind, and he
congratulated the author upon what he had put forward. He
thought, however, that a part of the information was not entirely
new. Still the species, he fully believed, was a new one, as several
of the characteristics are not found in any other described Plesio-
saur. He had an impression that the palatal foramina described
by Prof. Sollas were shown in the species described by Mr. Stutch-
bury fourteen years ago; and he believed they had been excavated
after that description had been drawn up. As to the Lacertilian
affinities of Plesiosaurus, he was unable himself, so far as he had
seen, to recognize any of importance. In some respects it had
affinities with Ichthyosaurs, Dinosaurs, and Crocodiles; so he thought
the Lacertilian affinities could not be pressed. Though he dif-
fered in some details, he thought the paper, as a whole, was done
extremely well.
ee
X ney
%
4
44)
i
4
}
i
\
t
as
APPENDIX.
*hexngonalis
*infraplanus
sp. -
top.
*gamma
}t§erandis
[:Bvansi (See
*tmacromeras
pachydoirus
teimplox (PA
} tttrochanteriv
| “ep.
*{tintorruptus
[Mansellii (Hulke)
‘megadeirus (Secley)
‘plicatus (Phil.), “allied to”
solidus (PAil.)
Prtosaunus (Owen).....
taequalis (Phil.) ..
§brachydeiras (Owen
Owen, MSS.) .
Owen)
Phil:
*nitidus (PAil)..
‘See
*tportlandicus (Owen)
‘Geontinuns (Otsen) ..
Lower Dias. |
Mippre Lis,
*ellipsospondylus (Oicen’
Fatt 2 )
Phil.)
Pontuanp Bens.
“carinatus (Phi) 1871 | Portland Rock...
*svinspitensis (Seeley) -s{ 1871 | Portland Limestone...
Onetackovs.
“Bornardi (Oiven) .. 1850 | Neocomian to Uppor Ohalk\
*constrictus ( Owen) 1850. | Chalk
§Gardneri (Seeley) 1877 | Gaul
*Platispinus (Owen), 1854 | Lower Greensand
*pachyomus (Owen) 1839 | Upper Greensand
*planus (Owen). 1864 | Grecnsand.
neocomionsis (Campiche) ..
ley) ..
il
storrodeirus (Seeley, MSS.
1s (Owen).
| Porrrrrononox (Owen) ....
(Owen)
Kimmoridgo Ola;
Kimmeridge Cla
Kimmeridge Clay
Kimmeridge Cla}
Kimmeridge Olay
Kimmeridge Olay.
Kimmeridge Clay ....-1++
Upper Greensand.
Lower Neocominn
Bottom of L. Greensand
Chalk
Kimmeridge Clay.
Kimmeridge Olay
Portland Limestone
Oxford and Kimmeridgo|
Olay and Coral Rog
Kimmeridgo Qlay..
‘Oxford and Kim. Olay
Shanklin Sand ...
L. Groonsand and Obalk ...
Upper Greensand, Lower|
‘and Middle Obalk
jptarsuntus (Oe) 1899 | Planorbis? .| Street, Bitton, Charlton ,
fbrachycephalos (Owen) 1939 | Turneri | Bitton; Bott...
; 1865. | Planorbis? -} Street... F
fede (Ss) 1881 | Obtusus ... 1] Obarmouth Restricted go
{dolichodeirus (Conybeare)... 1824 | Planorbis .. 4 Wein Ply Bristol, Bitton Type of genus...
li 1865 | Planorbis ? ,| Stroot... i
talien ( ) 1868 | Ostrea-beds
Tavki Oven 1838 Ostren-beds a q Lyme, Weston . Restricted genus
t Meeephalus (Conyea 1836. | Planorbis ‘| Street, Lymo, Weston .
reatromos (Quen) 1830 | Marl” Near Lymo
paesphalus (tule 1846 | Ostrea-beds, Streot, Wilmeote,
Pee tea (Oiven) 1865 | Bucklandi Oharmouth
Srost ea 2 a sa | CHSC)
Ae 1 lanorbis, Bucklandi ymo, Weston Erot
frugosus (Otren) Obtusus : §Grauby (Leicestershire), } a ee
saubtrigoous (Otcen) 1839 | Bucklandi? . Weston (near Bath)..
Oorwloy
Shot
Kimmeridge Bay
Ely.
Shotoyer
Shotover, Cumnor, Baldon
-] Quainton (Bucks).
.| Winspit (I. of Purbeck) ..
Reach, Arundel; Moscow.
Steyning (Kent)
ROLE E
‘| Tquaudon Quarry,
) Rea do)
:| Cambridge
:| Cambridge.
|| Ste. Croix; Moscow
‘|. of Wight
-| Burnham
.| Near Swindon, Shotover .
|| Market Raisin, Shotovor .
‘| Weymouth, Shotover .
‘| Shotover, Kimmeridgo,
yn:
vin
.| Shotoyer
.| Groat Grant
I. of Portland
Shotoyer
‘| Ohristian Maliord, Kimmeridgo,
RK
.| Bedfordshire -.
Maik
Cambridge, Frome, &e.; Moscow)
lay pils ...
Stanford,
over,
Murienosaurus
Colymbosauras
Elipsospondylic group
.| Colymbosaurus (Seeley 2)...
Manisaurus .,
Oambri
Moscow
sbury, near St. Neotts
ndon, Shotover
“Genus doubtful”
Or “now genus" (Ow. Kim,
‘oxcombe O. R.).
dstono, Sussex; Moscow ...
.| Owen, Brit, Ass. Rep. 1839, p. 82..
_| Hulko, Q. 3, GS; vol. xxvi. p. GLI
‘| Phillips, Valley o
| Seeloy, Q. J. G. 8. vol. xxxii
Owen, Brit. Ass. Rep. 1859, p.75.
Owen, Brit. Ass. Rap. 1839, p. 69,
Seeley, Ann. & Mag. N. H. eer. 3, vol. xvi. p. 352
Sollay} described Meco peer
Oren, Brit. Ass. Rep. 1859, p. 7
Capricornis . Saltburn Tato & Blake, Yorkshire Lins, p, 252,
Tamesoni |) Huntelit ate & Blake, Yorksbire Lins, p, 252.
Urren Dias,
*brachycophalus (Owen)... con 3 : , 2 York (Owe
iGrampin (Car § Baily) 863 | Upper part of Bifrons......] Kettloness (near Whithy) Carto &Thily, Dubi, Roy. Soa. Journ, peu
jlospandylus (sce) 1865) }| Communi =| puwntby, Owen, Pal. Soc., Linssie Rep. p. 12 Whitby
faubin (Lite f Blake) 1876 | Communi | 5 .| Dato & Blake, Yorkshire Lias, p. 24
thomalospondslos (Otcen) 1865 | Bifrons Whitby . | Owen, Pal. Soe., Linssio Rop. p. 1 ..]21, 80, 81, 33. ...| British, York, “Whitby .
Varma (ate & Blake) Whitby . “| mato & Blako, Yorkshire Lite». 250, apes a
et Lofthiouse Eretmosaurus 7? (T: § B.).| Sceloy, Ann, & Mag. N. H, ser. 3, vol. xv. p, 49 ......, 31. _} Woodvwardian
ae Whith: F . "| Tato & Blake, Yorkshire Lias, p. 24 }i9 :| Whitby
i s Eretmosaurus a| ri
4 | Lofthouse ‘ Rep, Yorksh, Phil, Soc. 1851 | York,
Lower Oouite. il 0 19
*qsorrations (PAilli Stonesficld Slate; Stonesfield Phillips, Valloy of Thame: iy
Tee Cee. Great Oolite . Minchinhampion Secley, Cat. of Rept. & Woodwardian.
Minpix: Oourre.
teurymorus (Phil. 1871 | Oxford Clay . Bedford ... % a Woodwardi
Sectsii gabe, ) 1874 | Lower Oxfurd Olay Huntingdonshire Muranosaurus (Slcy) Coll Eacds
osontensis (Phd) 1871 | Oxford & Ampthill Clay ...! Oxford, Long Marstoi Murmnosaurus
philarchus (Seley, 1869 | Oxford Clay Peterborough eee
*plicatus (PAIL) 1871 | Oxford Clay . ; * Bllipsospondylic group”
Knnrenainor Cray.
taffinia (Otven) « Kimmeridge Olay. Heddington, Shotovor Owon, B. A. Rop. 1839, p. 86 || Enniskillen, i
*brachistospondylus (Auk) Kimmeridgo Olay . Kimmeridge Bay ... Hulke, Q. J. @, 8. vol. xvi, p. 611
*brachyspoudylus (Otoen) .. Kimmeridgo Clay. Hedidington, Shotover, near Orvon, B, A. Rop, 1839, p. 78 || Oxford, Bristol, Woodwardian
Weymouth, Foxmouth
fdmdicomus (Oven), Kimmeridge Olay, Shotovor. Owen, B.A. Rep. 1899, p. 82.
Phillips, Valley of Thames, p. 37:
Phillips, Valley of Thames, p. 375.
Phillips, Valley of Thames, p. 375.
ley, Cat of Rept. & Birds, p. 97
‘Thames, pp. 873, 374.
Phillips, Valley of Thames, p. 370
Phillips, Valley of Thames, p. 374.....
Seoley, Ann. & Mag. Nat. Hist. cer. 4, vol. viii. p. 181
Phillips, Valley of Tham
Owen, Odontozraphy, p.
Phillips, Valley of ‘Thames, p. 359,
Owen, B. A. Rep. 1839, p. 83.
Phillips, Valloy of Thames, piste
Phillips, Valley of Thames, p. 360
Secloy, Ont. Rept. & Birds, p. 116
Owen, Pal. Soc,, Kim. Clay Rept. pt. 3, p.8
Phillips, Valley of Thames, p. £66",
Scoloy, Cut, RopseBirds, p_ 98
Owen, B.A, Rep. 1839, p85.
Seeley, Ann, & Mag. Nat. Hist. ser. 9, vol. xviii. p. 112)
Owen, Odontogeaphy, vol. ii. p. 19.
Owen, Odontogrephy, yol. ii. p. 19
10,
Dixon, Foss. Sussox, p. 396. .} 10,11, 12,15...) British.
Dixon, Foss. Sussex, p. 398. -} 11, 12.
Seeley, Q. J. G. S. vol. xxxiii. p. 541 liek oll. Gardner...
Owen, Ont. Foss, in Ooll. Surgeons, p. 6 ll. .| British.
Owon, B. A. Rep. 1839, p. 74... 41, 1 .| Woodwardian.
Owen, Pal. Soo., Cret Rop. Sup. 15, | Woodwardian, British,
Pictot & Campiche, Foss. Orét. de Ste. Oroix, ser. 2,| 11, 15. .| British, Woodwardian
EVAR riored
10, 11, 12, 15
wardinn,
..| Bristol (8 specimens) .
Woodwardian.
Bristol, British
..| British (8 specimens) ....
Woodwardian.
Jermyn Street.
British
Enniskillen.
Coll. “ Miss Phillpots” ..
Bristol, Warwick,
British ..,
§British,
(York?)
*Enniskillen, Bristol,
*Bristol.
Oxford,
.| British & Coll. Mansell.
.| Woodwardian.
Oxford ...,
British, *Bristol, Enniskillen, Wood-
.| With 2A
,| Syn. triatarsostinua (Haykins).
-| Quoted by Stutchbury as" macrourus.”
|] Tn beds with Anunonites heterophyllus,
.| Near Pl. dadicomus.
| With
..| Seo Oxford Oloy. It is doubtful whethor Phillips
To face page 480.
TABULAR SYNOPSIS OF THE GEOGRAPHICAL DISTRIBUTION OF THE PLESIOSAURS. BY G. F. WHIDBORNE, Esa, F.G.S.
. Tanre I.—English Species.
*=Vertebra. t=Bones of tho limbs, thorax, or pelvis. }=Skull. §=Skeleton, [—=Imperfoct skeleton. §=Toeth.
Date. Horizo Locality. Defined genus. Description. References. Museums, 4
Presiosavnvs (Conybeare) « 1821.
Ruetic.
etttas (Oman 1839 Owon, Brit. Asso. Rep. 1839, p. 80 . “Bristol.
*Hawkinsii (O1e" 5 ar Sco " Lowor Lins."”
rugosus (Otoen) « Eretmosaurus *Bristol ‘Seo " Lower Lins."
trigonus (Cuvier) ;
Figured in Geol. Trans. ser. 2, yol. v, p. 44 “Not
rom Whitby or Wurtemburg," Owen.
nchonella variabilis (Schloth.) and Ammo-
nites cbliquecostatus (Zict.) = A, semicostatus (1. & B,).
Soo Wright, Q. J.G-S. vol. xvi. p. 406,
Found with Ammonites planicosfafus, Sow. Min, Con.
148, ono of the most frequent Ammonites of the
Marston stone, as well as the Charmouth beds of
this zone,
\Bigured in Bridgwator Treatise.”
Tho most perfectly preserved specimen known.”
“Whitby,” Owen & Phillips, not Tato & Blake,
The Granby skeleton found with 4, stellaris,
|
thy,” Owen, not Tato & Blake, Soo Lowor Lins.
. below Dogger, with numerous Leda ctu.” |
porhaps belong’ to P, longirosris” (‘I. & B,).
“This is a synonym for P. macropferus, if tho latter is
an Kremosaurus.”
“Whit
“60
=P. grandipennis (MSS,).
Founded on a specimen labelled " macrocephalus.”
Sco Lower Lias,
A small species,
Am. Duncani, Lamberti, &e. Itis tho sano spe-
cimen ag the“ Plesiosaurus grandis?" of Phillips,
n
Valley of Thames, p. S18.
“Syn. Pl. recentior? (Qonyb. & You Meyer), and Pl,
gigantews? (Gonyb. 1824),” Owen,
makes (wo ord single species here,
Small yortobran, probably but not cortainly from Port:
Jand Rook, Tt Ouyier's nawo stands, this should bes
como Pl, Phillipri.
“Tt approaches H, megadaters! Sooloy.
Coll. Leo.
Coll, Swith.
Oxford.
..| Oxford, Woodwardian...
Oxford.
Oxford, Bri
Woodwardian
Oxford.
Woodwardian.
British.
Oxford.
Woodwardian.
Enniskillen, Oxford, British.
..| British.
11, 12, 15 ¢..) Woodwardian,
«| ‘Tho largest long-necked Plesiosaur known.
Syn. "Pl, mamillatus (Owen).
“Found with Am. vertebratis, whioh, howovor, occurs in|
Uppor Oxford Olay at Cowloy,” Phil,
Fouud with Arm, Duncani, Lamberti, &o.
Tanre I.—Foreign Species.
Pestosavnus.
jonensis (Zen
Nordmanni (
Bp. -.
indicus (Lydekker) .
i
B
pentagonus (Cue).
profundus (Zonk
suoyicus (Quon.)
Norr.—Hawkins, in (6),
Stercosurw
complete li
Omitting the most uncertain species, Table I gives 23 Rhuctio and Lisssie, 4 Oolitic, and 9 Oretaccous—making a total of 63 English species hitherto named or described. ‘There is, however,
1836,
2) from
S24.
182:
1838,
1839,
1540.
1s41,
1846, Stutchbury, Q. J. G. S,, vol
1848.
1851.
1850, Owen, in Dixo
Exasuosxonvs.
; : Owen, Brit. As. Rep. 1801, p. 122 -... 26 Ta : : Seoloy, Q. J. G.8. vol. xxii. p. 5Al.
1525. | Oolite: Gur. Os. Foss. vol: p. 496, 9. “Provisionally veers (Cone) Niobsars, +} Cop, Bull. 0.8, Sury.vol iit no. 9, p.600,
| Bay. of Concepcion Blake, Geol Mag 1803.” named,” Ouv,
’ Waipara Bods (Australia) | Owen, Geol. Mag. vol, vii. p.49. Ma ;
isin Neen » | Bich: Bull, de Moscow, 1846 Trasali (lector) Orelacoous,.....s.| New Zealand. rma, NZ, Inet, vol, vis p40) sven (99,
as Owen, Geol, Mog. sol. vii. p.0, [p-30]
eae Bydckker, Rep. Geol, Surv. Ind. vol. x] Puroasvnce- a ‘
if E Zauk. Beitr, rw. p. 65 Dedsbyspondslus (Oven), Wo |lerieecary .| DBichwald, Lethean Rossies, p, 1260 | Probably anerror’?
1859? | Gris Neooom. Orimea D'Eichwald, Lethwa Rossi = % |) 15
isp Honfleur, Cayier, Os. Foss. vol Worrinshit (Fisch). val 1616. | Neocomfan +o] Kiach. Bull, de Mfoscou,vol.i. pp. 11, 105) 10,
Zenk. Beitr. Urw. 64, t. 6
a i Quonstedt, Der Jura, pp. R 4 P
1828 | Hample Zone | Hillisusen: Quenstedt) Dor Jura, t. 58. f. 3. NgSTE 1867 | Neocomian Fisch, Bull. do Mosoou, vol. i. p. 902.) 16,
: 3 regoing Lis 16. 1861. Owen, Brit. Assn. Rep. p. 129, 9. 1876. Phillips, Geology of Yorkshire, od. 2.
Books and PADIS ee a | 17. 1561-69. Owen, Bal. Soc, Kin, Clay Rept BI. 1875. Tate and Blake, Geology of Yorkshiro. .
Conyb. Geol. Trans. ser. 2, vol. i. p- 103. On Pi. dolichodeirus. 18. 1861-70. Owen, Pal. Soe., Linssio Rept, R BE SF. Soy) Q UG: 8 vo, pH, on Muh Gardner p 710,08
Her, Os. Rosa. vol 19, 1866. Carte and Baily, Dublin Roy, Soc. Lip, p.160. On Pl Oramp- rl, Beatie .
Perisena Berdgowater ‘Treatise. On Pl. macrocephalus &o. toni. vs CE SeNE ROMS eae 83, 1878. Wright, Lias Ammonites.
Owen, Geol. Trans. eer. 2, yol. v.
Owen, Brit. Association Rep. p-
Hawkins, Great Sea-Dragons.
Owen, Brit, Assn. Rep. p. 60.
Bronn, Index Pal.
Owen, Brit \- Rep.
Foss. of Sussex.
1858. Quenstedt, der Jura. Phe am
1859. D'Eichwald, Lethaa Rossics, vol. ii, sect 2
has two fino figures; but his names being generic and o
© Rhatic, Placodus (coll. Moore) and Tanys*ropheus (coll.
16. On Pl. macrocephalus.
i. p. 411. On Ph megacephatus,
a
Viant). "Owes’s ‘Walzontology’ and Von Meyer's Palasontographi
1864. Geol, Mng. p. 47.
Sceley, An. Sf. N. H.
. xvi, p. 352. On Pl,
Geol. Mag,
7. Moore, Q-
Mansellix.
on the PI
rently merged by Oren in his Report (1890 and 1841), it
rp. 144.
FG.S, vol. xii p. 448, Abnormal Secondary Deposits.
). Hulke, Q J. G.S, vol. xxvi. p. O11. On Pl. brachistospondylus aud
Seeley, Woodwardian Ostalogue of Rept. and Birds.
). Owen, Geol Mag. vol. vii. p.49. On
Phillips, Valley of Thames.
Seeley, An. MLN. H.
or QI.G.S vol. xxx. p. 197, on Murenosaurus
lesicsaurian Pectoral Arch.
49 & 992. On Pl, macropterus.
sor. 8, vol. xv,
Phi. cliduchs.
eleutherazon &
farians from New Zealand,
ser. 4, vol. viii, On Pl. winspitencit. e
Toe ee uras Leedsit; p40,
has not
ica” give many other foreign species and genera from
been poreible to refer to them in the tables. Prof. Seeley,
Notices of Plosiosauri alsa occur in the following works.
1821, Do la Becho and Conybeare on Plesiosaurus, Cool. Trans. sor. 1, vol. vs p. O11.
1837. Pusch, Polens Paliontologie (?).
1546-47. ns alas do Moscou.
1850, Owen, Odontography. .
Gay, Historia iia y politics de Chile,
1859. Pictet et Campiche,
1858. Lucas Barrett, An. & Mo
180. Owen, Palaontolozy.
1874. Hector, New-Zealand Inst. vol. vi.
N. IL 1808,
1876. Lydekker, Rep. Geol. Surv. Tndia, vol. x.
in Q J.G.S, vol. xxxili. p. 442, notes the fol
the European ‘Trias.
‘here are ssid to be Done from that of America. Table II docs not aim
Fossiles da torrain Orétacé des environs de Sto. Croix.
p00.
Greensand,
, : bridge
lowing. genera :—{1) from the Cambridge Gromer
at present no reason to suppose that some of the names 8r® not synonyms,
abana taney
a ahd Khe Nth ce
ie. aor Pert> aN 4
KU Lis a hake Ries 7 Oe PE
ae Fe
is: F
5 ie
in)
4
hy
i
Fa
;
a
MEGACEPHALUS AND P. BRACHYCEPHALUS, 481
Prof. Sorzas expressed his sense of the generous way in which
Prof. Seeley had spoken of his paper. It was impossible to write a
paper without making use of material already published; but he
thought that there was but little put forward as new which was
not really so in his paper. He thought the Lacertilian affinities
were extremely well marked in the skull of Plesiosaurus. His de-
termination of the structure of the anterior part of the roof of the
mouth in P. megacephalus confirmed him in this opinion.
482 H. HICKS ON THE REMAINS OF PLANTS FROM THE
37. On the Discovery of some Remains of Prants at the Base of the
DENBIGHSHIRE Grits, near Corwen, Norra Wares. By Henry
Hicks, Esq.,M.D.,F.G.8. Wirthan Appendix by R. Krueriper,
Esq., F.R.S., Pres. Geol. Soc. (Read May 25, 1881.)
[Puats XXV.]_
In August 1875, when searching for fossils in the Pen-y-Glog
slate-quarry, which is situated about two miles to the east of Corwen,
I noticed some carbonaceous-looking fragments and markings on the
shales in association with the massive grit beds towards the top of
the quarry, which I thought at the time might possibly be plant-
remains. Last summer I had another favourable opportunity of
examining these beds; and I was fortunate enough to discover
undoubted plant-remains scattered very abundantly over their
surfaces. I submitted these for further examination to Mr.
Carruthers, of the British Museum, and had the satisfaction to
find that he entirely confirmed my views as to their nature. He
said they were undoubtedly “ angular fragments of plants,” but that
the specimens were not in a sufficiently satisfactory condition to
determine the actual plants to which they belonged. I decided,
therefore, not to bring the matter before the Society until I had
another opportunity of visiting the quarry and of endeavouring to
procure more perfect specimens. This I was able to do lately;
and the additional materials now found have proved to exhibit
structures sufficiently well marked to enable a very clear identifica-
tion of several distinct plants to be made out. The specimens have
been generally examined by Mr. Carruthers, and some specially
by Mr. Etheridge and Mr. Newton, of the Jermyn-Street Museum.
Amongst them have been found numerous small spherical bodies
identical in general appearance, and in internal structure, with the
Pachytheca described by Sir J. D. Hooker, from the bone-bed at
the top of the Ludlow series. These are supposed to be the remains
of spore-cases of land plants belonging to the order Lycopodiacee ;
other specimens are supposed by Mr. Carruthers to be the micro-
spores, and others to be fragments of the stems of the same plants.
Some of the specimens would indicate the presence also of plants
belonging to the genus Psilophyton. These, though tolerably abun-
dant, occur chiefly as carbonaceous markings, and show little evi-
dence of structure. The combined results are sufficient to make
it clear that we have here a terrestrial flora of a tolerably high
order. The majority of the fragments, however, belong to a curious
plant not hitherto found in Great Britain. It was first discovered
by Sir W. Logan in the Devonian rocks, in the peninsula of Gaspé,
Lower Canada, and described by Dr. Dawson, of Montreal, in the
Quart. Journ. Geol. Soc. for 1859, under the name Prototaxites.
Dr. Dawson described it as a land plant of large size, belonging
Mmtern Bros, mp.
Sees a
ss
Fem acetone BE
C
Oo.
8.
REMAIN,
SO rere
etary oe
9°
I
SILURIAN PLAN
X 200
ile
os
sooner it
Quart. Journ. Geol. Soc Vol XXXVI TP:
ith.
4A.S Foord
ai
bie a, y
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES. 483
to the Conifer, but yet differing from any Conifer known to him
“in the cylindrical form and loose aggregation of the wood cells, as
seen in the cross section, in which particular it more nearly resem-
bles the young succulent twigs of some modern Conifers than their
mature wood.” He maintained, however, that it was an “ exogenous
tree, with bark, rings of erowth, medullary rays, and well- developed
though peculiar woody tissue ”*,
Mr. Carruthers subsequently examined the same plant and re-de-
scribed it in an elaborate paper in the Monthly Microscopical Journal
for October 1872, and gave numerous reasons for excluding it not only
from the Conifer, but from land plants altogether, and for placing
it in preference among the Algze. In doing so, however, he said it
was an “anomalous Alga, and, indeed, that with the materials
known, it was not possible to correlate it with certainty with any
known group of Alge.” The identity of our plant with the above
mentioned, which was re-named by Mr. Carruthers Nematophycus,
is placed beyond doubt by the following note kindly given me
by Mr. Carruthers :—
‘«‘ The slides prepared by Mr. Newton show clearly that his deter-
mination of the fragments of charcoal and petrified remains of plants
in the Silurian rocks which you have found, belong to the same type
of plants as that discovered by Logan at Gaspé, in beds which he
considered to be of Devonian age. This was described by Principal
Dawson in the Quart. Journ. Geol. Soc. (vol. xy.) under the name Pro-
totaxites Logani. I made a careful examination of specimens which
I owed to the kindness of Dr. Dawson, and published the results of
this examination in the Monthly Microscopical Journal, giving the
reasons for placing it among cellular plants and naming it Nemato-
phycus Logani. The specimens show very distinctly the larger
tubes of Nematophycus, running generally in a subparallel direction,
but passing in and out amongst each other. The walls are not in juxta-
position, leaving free space all around them, which was occupied, as
is shown in the better-preserved specimens from Gaspé, with a dense
tissue of more delicate tubes of smaller dimensions. That your speci-
mens belong tothe plant called Nematophycus | havenodoubt. The
conditions under which they are found are very different from those
described by Dr. Dawson. His specimens were large trunks, some-
times perfectly silicified and preserving their most minute structures.
Your specimens, consisting of small fragments, consequently supply
no help to the further knowledge of this remarkable plant, unless
the occurrence on the same slab, in tolerable abundance, of small
round bodies having the same form and structure as those found in
the Ludlow bone-bed, which were figured and described by Sir J.
D. Hooker under the name Pachytheca, indicate some possible re-
lationship. The specimens found by you are perhaps smaller than
those from Ludlow. ‘They present no indication of attachment, and
no evidence of their relation to Nematophycus, except their being
found together, which is not always a good basis for structural re-
* * American Naturalist,’ vol. v. p. 249.
484 H. HICKS ON THE REMAINS OF PLANTS FROM THE
lations in fossil plants. The minute bodies, aggregated together,
which you have also shown me are, I believe, spores; and as they
are united in threes, they agree with the forms of the microspores
of Lycopodiacez, both recent and fossil, and testify to the existence
of a dry-land flora. Perhaps some of the anthracite fragments may
belong to the stems of the plants of which these are the reproductive
organs. The ribbon-like carbonaceous impressions, with a slender
axis, must have been also dry-land plants ; they remind me of the
plants discovered and described by Principal Dawson, C.M.G., as
Psilophyton.
“W. CARRUTHERS.” |
The specimens found, hitherto, of Nematophycus are all in a frag-
mentary condition, the largest pieces being generally under 2 inches
in length, and a little over half an inch in thickness. The natural
outline, however, is frequently preserved ; and if the majority of the
fragments are any guide to the natural size of the mature plant, it
is evident it must have been small as compared with the Devo-
nian one of Sir W. Logan, which attained to over a foot in diameter.
That the plant must have been plentiful at this early period is clear
from the very great abundance of the fragments in some of the beds ;
sometimes so closely compressed together are they, that they form
an actual carbonaceous seam from one to two inches in thickness.
The microscopical characters of this plant, which are peculiarly
interesting, will be fully referred to in the Appendix by Mr.
Etheridge *.
The discovery of Pachytheca and other spore-like bodies in con-
siderable abundance in association with Nematophycus is curious, but,
as remarked by Mr. Carruthers, is no direct evidence of their relation-
ship. We know, moreover, from geological evidence, that the shore-
line at the time could not have been very far distant, and therefore
that it is quite possible there may be here a mixture of marine and
dry-land plants. ‘The broken condition of the specimens also tends
to show that none of them lived in the actual positions in which they
are now found, but that they were brought here by some accidental
cause, possibly along with a great amount of sediment, and as the
result of river-floods, or of depression followed by rapid marine
denudation. |
The almost abrupt appearance at this horizon of massive beds
of grits upon fine muddy deposits of considerable thickness, such
as the slates immediately below, evidently tends to show that a
physical change was then taking place in some neighbouring area ;
but besides this there is nothing to indicate a physical break at this
point.
* Dr. Dawson, in his reply to Mr. Carruthers, ‘Monthly Microscopical
Journal,’ 1873, still insists on his former diagnoses; and in a letter addressed
to me, dated June 16th, 1881, in reference to the published abstract of this paper,
says :—“ I have perfect confidence in my genera Prototaxites, Nematoxylon, and
Celluloxylon, as representing primitive types of land plants; and I maintain my
judgment as to these genera, and I believe it will be vindicated by future dis-
coveries.
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES. 485
In addition to the above-mentioned tolerably well-preserved plant-
remains from the shales associated with the grits, there are un-
doubted evidences of a still earlier and probably equally important
flora in beds of slate at the base of the quarry. Instead, however,
of the remains being preserved chiefly in the condition of mineral
charcoal, as in the upper beds, they occur here mainly in the state
of a very pure anthracite. At the same horizon some large nodules
are seen ; and in the centre of these anthracite is also occasionally
found, evidently forming the nucleus. From some of the specimens
examined, I conclude there can be no doubt that these plants must
have been of considerable size; and the amount of carbon left on
some of the surfaces, apparently from a single fragment only, would
tend to show, as suggested by Mr. Carruthers, that it must have been
derived from vascular plants. There can be little doubt, therefore,
that there is in the slates and nodules, even in the so-called Taran-
non slates, very clear evidence of a terrestrial flora of considerable
importance*. The anthracite, as now found, is usually broken into
innumerable small fragments; but it is perfectly clear that this must
be due to changes to which it has been subjected since it was de-
posited—changes which also produced induration, cleavage, and frac-
tures in the argillaceous sediments. ‘The fissures in the anthra-
cite, and in the charcoal in the other beds, are generally filled by a
fibrous mineral, which occurs here in some places in considerable
abundance. Mr. T. Davis has kindly examined this, and says that
it is a “ fibrous form of a hydrated magnesian silicate.” In other
cases the fissures are filled with calcite.
The difference in the conditions of fossilization in which the
remains are now found at the two chief horizons may doubtless be to
a great extent explained by taking into consideration the manner in
which they were imbedded in the deposits. The thick grit-beds were
evidently thrown down rapidly, and covered over the fragments before
decomposition had taken place in them to any great extent. The
fine muddy deposits which compose the slates were evidently thrown
down much more slowly, and in a tolerably quiet sea ; therefore vege-
table material resting on the bottom would have time to decompose
almost completely before it would be sufficiently covered over by the
deposits. ‘To a certain extent the same cause has allowed remains
of vascular plants only to be preserved, as cellular ones would be too
readily and too completely destroyed to show indications of their
presence in such deposits. This is, I believe, the reason why re-
mains of Algee are not more frequently found in these older rocks,
and why impressions only are seen in most cases.
The Pen-y-Glog quarry, where the specimens were obtained, has
* Since this paper was read I have received from Mr. Phillips, the manager
of Pen-y-Glog quarry, to whom I am indebted for much assistance, specimens
which show clearly that plant-remains occur in the pale shales below the Den-
bigh-grit series in the same state of preservation as in the beds at the top of
the quarry. These shales also contain numerous calcareous nodules.
Oey. G.0. No. 147. 2%
486 H. HICKS ON THE REMAINS OF PLANTS FROM THE
been already referred to in several papers read before this Society ;
and its geological position is therefore well known. In the Survey
maps and sections its horizon is given as immediately at the base
of the Denbigh-grit and Flag series. It is shown to be separated
from the Bala or Caradoc beds by only a very thin band of shales, which
also contain plant-remains. In the published sections across this
neighbourhood approximate thicknesses of between 4000 and 5000 feet
of beds belonging to the Denbighshire-grit and Wenlock series are
shown to occur in direct superposition to the beds in which the plants
are found. None of the beds belonging to the Ludlow series are
mentioned as occurring in these sections, the highest given being
Wenlock : hence, if the former were deposited in this area, they have
all been since removed by denudation.
The geological horizon of the plant-yielding beds in relation to
typical sections in other areas is rather difficult to define, since
hitherto the Denbighshire-grit series has not been satisfactorily
correlated with any other group. In the Survey sections the true
Wenlock beds are made to come in at an horizon somewhere about
2000 feet above these beds, and to occupy the remainder of the sec-
tions. ‘The only beds below the plant-beds which have been actually
correlated by their fossil contents with those in other areas are the
Bala and Lower Llandovery beds; hence, at present, the evidence
goes to prove that they must be older than the Wenlock, and newer
than the Lower Llandovery. In Mr. Ruddy’s paper* the Lower
Llandovery beds are said to be represented in this area by the Corwen-
grit series of Prof. Hughes; and the latter, in summing up the
evidence as to the succession in this section, says 1t goes to prove :—
‘that the Corwen grits are distinct from the Pen-y-Glog grits ; that
there is more evidence of a discordancy at their base than at the
base of the pale slates or the Pen-y-Glog grits; that there are
generally some beds of conglomerate, sandstone, or limestone with
sandstone on the horizon of the Corwen grits; that the general
facies of the few fossils obtained from these beds in the district
examined is that of May-Hill rocks”.
He states, further, that these Corwen grits are succeeded by beds
which ‘ pass up into the ‘ pale slates’ of the Survey, which in turn
pass up into the striped flaggy beds of Pen-y-Glog, on the top of which
come grits, to be referred to the true Denbigh Flag and Grit series.”
As the latter are the higher beds mentioned where plants were
obtained, we have ample evidence of their position in regard to the
succession exhibited here, both from beds below and from those
which rest upon them. In other areas the position occupied here
by the Denbighshire flag and grit series, the pale slates, and the
Corwen grits seems to be chiefly filled up by the Llandovery or May-
Hill group and the Tarannon slates: the latter, I think, with the late
Mr. Salter, however, should always be included in the May-Hill
* Quart. Journ. Geol. Soc. vol. xxxv. p. 200.
t Ibid. vol. xxxili. p. 207.
437
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES,
Diagram Section from Nant Liechos, near Corwen, to Moel Morfydd. (Horizontal scale 1 inch to a mile. Vertical scalo
about 3000 feet to 1 inch.)
S.W. 3 N.E.
Poviuion of slates
of Pen-y-glog :
slate-quarry. Dee river. Moel Morfydd.
RSE eA CER RB
1. Bala beds. 5. Wenlock series.
2. Corwen Grits and Shales (Lower Llandovery). x Chief positions of plant-remains.
3. Pale slates. i Base of Upper Silurian of Survey.
4. Denbigh Grit and Flag series.
N
be
N
488 H. HICKS ON THE REMAINS OF PLANTS FROM THE
group. The accompanying section (p. 487) will explain more fully
the succession in this area and the actual position of the chief beds
containing the plant-remains.
The evidence of the geological horizon, derived from the fossils, is
at present imperfect; for the animal remains found in the slates, j in
association with the plant-remains, are chiefly Graptolites, though
fragments of Hncrinites, species of Orthoceras, and some Brachiopods
are occasionally found. The following species of Graptolites were
recognized by Mr. Hopkinson, in a collection made by him and my-
self at different horizons im this quarry in 1875, viz. Cyrto-
graptus Murchisom, Monograptus priodon, M. Sedgwicku, M. ake
M. vomerinus, M, Hath, and Retiolites Geitzianus*.
These forms, he considered, were ‘characteristic of beds 6 the
summit of the Coniston Mudstones, or base of the Coniston Flags ”’
in the Lake district. The abundance of Graptolites found in these
beds would tend to show that the deposits, for the most part, were
thrown down in a tolerably quiet sea.
It seems, therefore, so far as the evidence can be read at present,
that this immediate area was not greatly affected by the physical
changes which occurred in the neighbouring areas at the close of
the Bala epoch—that if uplifted above sea-level, it must have been
previous to the deposition of the Corwen Grits, as shown by Prof.
Hughes. The physical break, therefore, if it exists here at all, must
be placed at that point, and not, as formerly supposed, at the base of
the so-called Tarannon Shales. There is, however, no visible uncon-
formity between the Lower and Upper Silurians anywhere in the
sections in this neighbourhood; and it is quite possible that the area
may have remained under water during the whole of the Mid-
Silurian epoch+. The parts raised above sea-level were chiefly to
the suuth-east, south, and north-west of this area. JI am inclined to
think that there was not a very extensive land area, but numerous
islands, some of them of volcanic origin. They reached undoubtedly
as far as Shropshire to the 8.E., and to Caernarvonshire (and probably
beyond it) to the N.W. There is no satisfactory evidence to show
that they extended much further to the 8.W. than the neighbour-
hood of Builth, as the deposits apparently accumulated uninter-
ruptedly during this time in part at least of Caermarthenshire, in
Pembrokeshire, and in Cardiganshire. This is the only way in which
we can account for the presence in those areas of some thousands of
feet of beds between the topmost Bala and the Wenlock series, and
* Mr. C. Lapworth has also kindly examined a small collection made by me
recently in the same quarry, and mentions the following forms as recognizable.
They were chiefly collected from the middle bands of slate and above the beds
with nodules and anthracite:—Letiolites Geinitzianus, Cyrtograptus Murchisont,
Monograptus vomerinus, M. personatus, M. priodon (and vars. riccantonensis,
Lapw., and Flemingit, Salt.). He states, as to the correlation of these beds with
those in other areas, that, so far as the evidence derived from the above Grap-
tolites can be made out, they would occupy a position equivalent tothe ‘‘lower
zones of the Wenlock shale of Shropshire and the west of England.”
+ See paper by author, Brit. Assoc. Report, 1875.
*
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES. 489
their almost entire absence in the Longmynd and other districts.
For the same reason also it must be expected that a great diversity
will be shown in the sediments belonging to this period in ditterent
areas, and particularly so in proportion as they approached to or
were distant from any of the raised parts. The fauna would also
in consequence vary considerably. Jor these reasons it becomes
difficult to correlate with any satisfaction all the beds which are
found between the Hirnant limestone of the Bala epoch and the base
of the Wenlock, which are known in different places chiefly under
the name of Llandovery or May-Hill, or Tarannon, and in the area
under consideration as the Denbigh Grit and Flag series. The con-
clusions, therefore, arrived at in regard to the plant-remains and the
geological horizon in which they are found are :—that theage of the
beds must be somewhere between the base of the Wenlock and the
Lower Llandovery, probably not far from the horizon of the May-
- Hill beds (Mid Silurian) ; that the plants did not live on the surfaces
on which they are now found; that their position here is an acci-
dental one; that they were not brought from a great distance, as
they occur at several horizons; that the shore-line from which they
were derived was towards the south or west; and that the land
areas were chiefly formed towards the close of the Bala epoch.
If we compare these plant-remains with those discovered in lower
Paleozoic rocks in other areas in this country, we do not find so im-
portant an assemblage anywhere so low in position, certainly not at
a lower horizon than the Upper Ludlow rocks, and probably not
below the Devonian. It is probable also that an equal number of
important plants have not been found together at so low a geological
horizon in any other part of the world. Those found in the Silu-
rian rocks elsewhere are :—the branch of a fern, described by Count
Saporta under the name of Hopteris Morieri, discovered by Professor
Moriére in the Middle Silurian at Angers, France; the Glyptodendron
of Prof. Claypole, from the Clinton group of Ohio, America; and the
species of Psilophytum, Annularia, and Sphenophyllum described by
Prof. Lesquereux, also from the Silurian rocks of Ohio. It is a
curious fact that in each of these areas, in Britain, France, and
America, the land plants are in a greatly broken condition, and
occur in association with a marine fauna.
Their geological position in each country seems to bear out the
view that physical changes were taking place almost contempora-
neously in Britain, in parts of the continent of Europe, and in
America at this time. These changes, which took place towards
and at the close of the Lower-Silurian (Ordovician) epoch, caused
land to be formed in each of these areas of greater extent than_
could have existed since the earliest Cambrian times; therefore
it is probable that unless we find land plants in the lowest Cambrian
deposits, we are not likely to meet with them in the intermediate
groups, which appear to have been deposited upon each other unin-
terruptedly. That there were periods of shallow water, when de-
posits were thrown down nearly at an equal rate with the depression,
490 H. HICKS ON THE REMAINS OF PLANTS FROM THE
is certain ; and marine plants probably lived in abundance. The cel-
lular structure of the marine plants, however, rendered them so
readily liable to decomposition, that it is not much to be wondered
at that their remains are seldom found. ‘The various markings
which have been attributed to land and marine plants in the earlier
rocks may in some cases have been produced by them; but others,
as shown by Salter, must have been tracks produced by worms.
Of the most important of those about which doubt still remains may
be mentioned Hophyton of Torell, from the Lower Cambrian rocks
of Scandinavia, but which I have also found at St. David’s. Cruziana,
from the Lingula-flags of North Wales, supposed by Salter to be a
worm-track, I believe, from evidence I have been collecting for some
time, will prove to be an Alga. Buthotrephis, found in the Lingula-
flags and in the Arenig rocks in Wales, and by Prof. Nicholson in
the Skiddaw Slates of Cumberland*, but first discovered and de-
scribed by Prof. Hall in America, appears also to be allted to the
Algee. Ot Hophyton? explanatum, which I found in the Tremadoc
rocks of St. David’s, I fear the evidence is scarcely sufficient to ally
it with land plants. Its strong tubular structure renders it unlike
any known land plant; and the only other fossil found yet to which
it can be compared is the Pyritonema of Prof. M‘Coy, placed by him
amongst the Zoophytes, though its true nature is still a matter of
much doubt.
Appendix. By R. Erurriver, Esq., F.R.S.. Pres. Geol. Soc.
Karty in the present month Dr. Hicks brought for my inspection
several slabs of micaceous sandstone, having upon their surfaces
numerous fragments of carbonaceous matter, which possessed no
definite shape or apparent structure. Their general appearance, in
some cases, was that of decomposed coniferous wood, in others,
resembling bundles of finely striated black or dark-brown carbon,
brittle or tough, the black portions being by far the most brittle ;
the lighter and darker remains, however, undoubtedly belong to the
same plant, but differently mineralized. Hitherto, in Britain, no
true plant-remains are known to occur below the Upper Ludlow,
and the only recognized species in that formation is Pachytheca, or
Pachysporangium. Between the Upper Ludlow and the base of the
Denbighshire Grits no traces whatever of plant-remains have yet
occurred in British Silurian strata.
Dr. Dawson, as far back as 1859, in his paper upon the “ Fossil
Plants from the Devonian Rocks of Canada’’}, described, amongst
* The fossils formerly placed by Prof. Nicholson in the genus Buthotrephis,
from the Skiddaw Slates, have been since redescribed by him and Dr. Dawson
under the generic name of Protannularia.
tT Quart. Journ. Geol. Soc. vol. xv. p. 484.
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES, 491
other things, a new genus which he called Prototaxites, and the
species Loganz; he considered this to be the oldest known fossil
tree in America, and, as such, gave it the name of Prototaxites,
believing that it belonged to the Taxineee. Subsequently (1863), in
vol. xix. of our Journal, he described other fossil plants from the
Gaspé Devonians ; and apparently the same or a similar fossil is again
described under the name of Nematoxylon crassum.
Specimens of this plant (Prototaaites) were subsequently examined
by Wm. Carruthers, Esq., F.R.S., who pronounced it to be a colossal
Alga, or seaweed, and named it Nematophycus. Mr. Carruthers
published an important paper upon this plant, wherein he gives his
reasons for widely differing from Dr. Dawson *.
Immediately on the receipt of Dr. Hicks’s specimens, and knowing
how large a problem depended upon a right interpretation of the
structure and affinities of the plant-remains, through their strati-
graphical position or age, I at once obtained Mr. E.'T. Newton’s aid in
preparing microscopical sections. The result has been in the highest
degree satisfactory ; and he at once determined these remains from
the Denbighshire Grits of Pen-y-Glog to be the Nematophycus of
Mr. Carruthers.
Mr. Newton and myself have microscopically examined several
sections of both the lighter and darker portions of the carbonaceous
matter placed at our disposal by Dr. Hicks; and we feel convinced
that they both present the same structure, the difference seen being
almost wholly due to the fact that the intensely opaque nature of
the carbonaceous matter in the darker specimens obscures the
structure. Mr. Newton’s observations were therefore made upon
the light-coloured specimens, which we have carefully examined
together. When examined with transmitted light and with a low
power, the fragments show that the fibrous appearance is due to
a number of dark rod-like tubes or cells running in a longitudinal
direction, but in a more or less vermiform or wavy manner, some-
times closely packed together (fig. 2), sometimes more widely
separated: these tubes or cells have one general direction, and
consequently appear nearly parallel; but closer examination shows
that other cells irregularly curve in and out of plane, and are not
parallel.
In many parts a dark and apparently granular substance seems
to fill the tubes, and may be resolved into round globules varying in
size (fig. 3).
In certain favourable spots some of the tubes appear to be crossed
by very fine transverse lines (fig. 4) which strongly resemble spiral
fibres ; these lines, however, may be due to the nature of the mineral
which fills the cells. On others a network of fine lines may be
seen spreading over the tubes; these might be thought accidental
but for their frequent occurrence. In transverse section (fig. 1) the
* Trans. of the Royal Microscopical Soc., Monthly Microscopical Journal,
1872.
499 H. HICKS ON THE REMAINS OF PLANTS FROM THE
cells are more or less circular, and are separated by greater or less
interspaces in different parts of the section.
Compared with the Nematophycus Logani as figured by Mr. Car-
ruthers, the minute structure of these carbonaceous fragments will
be found to agree precisely, with the one exception that the finer
tubes or cells filling the interspaces between the larger ones, which
Mr. Carruthers figures and describes in Nematophycus, are not so
distinct in Dr. Hicks’s specimens. The double spiral fibres figured
by Dr. Dawson when he first deseribed his Prototavites (= Nema-
tophycus, Carr.), are rather to be referred to the interlacing cells
(network in Pen-y-Glog specimens) than to the fine spiral fibres
seen in the latter (fig. 4).
The rounded seed-like bodies found with the carbonaceous frag-
ments are hollow and thick-walled. In microscopical sections the
wall is found to be composed of radiating fibres (cells ?) arranged
nearly parallel to each other and slightly wavy (fig. 8). These cells
are irregularly filled with spore-like bodies. The seed-like bodies
resemble the Pachytheca from the Upper Ludlow beds both in
their outward form and in the radiated structure of their walls.
The question naturally arises, Are the carbonaceous fragments
so well known to occur in the Ludlow bed (Downton sandstone) of
the same nature and structure as the Denbigshire-grit specimens ?
Mr. Newton has not been able to obtain transparent sections of the
Ludlow woody specimens; but, from what little we have been able
to make out, these Ludlow fragments likewise show tubular struc-
ture, but not quite of the same character as those from Pen-y-Glog.
On first seeing. Dr. Hicks’s specimens I pronounced the remains
to be those of some marine Alga; but I was not then acquainted
either with Mr. Carruthers’s paper on Nematophycus or Dr. Dawson’s
description of Prototavites, neither being then known as British
plants; and no opportunity had occurred to me for examination.
The sections made by Mr. Newton reveal in the most perfect and
satisfactory manner the innumerable vermicular cellular filaments
which constitute nearly the entire structure of what must have been
the stem, and also the dense spongy nature produced by the smaller
tubes, which seem to ramify irregularly. The larger tubes are not
strictly parallel to each other, although they run in the same general
direction ; they appear to be continuous, and their ends bluntly
rounded.
The description of the structure of Nematophycus, and the discussion
of its affinities with certain orders in the Chlorospermee, are so ably
and completely done by Mr. Carruthers, that little is left for further
description, especially as there is no doubt whatever that the plant-
remains in the Denbighshire Grit from Pen-y-Glog are unques-
tionably Nematophycus of Carruthers, and the Prototaaites and
Nematoxylon of Dr. Dawson, referred by Dr. Dawson to the Conifere
through the Taxines or Yews.
The fragments, small as they are, show unmistakably that we
have at this low horizon the Gaspé plant (Prototaaites) which occurs
in the Devonian rocks of America. ‘This is an important fact, as
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES. 493
the so-called Fucoidal remains are mere impressions, and many, if
not all, are trails or burrows of Annelida.
The interest at first attached to these special remains was centred
in the hope that they were portions of terrestrial vegetation grow-
ing on a contiguous land surface during the deposition of the Den-
bighshire Grits. Now, however, we have clear evidence that these
remains, to which we more especially refer, formed portions of a
colossal seaweed whose habit resembled that of the North-Pacific
species of the genus Nereocystis and the arborescent JLessonia,
and probably, as Mr. Carruthers suggests, the Macrocystis pyrifera,
which attains the length of 700 feet. The arborescent Lessonie,
belonging to the natural order Laminariaces, form large submarine
forests, the stems of which, when dry, resemble exogenous wood,
owing to a false exogenous growth. ‘This pseudo-exogenous struc-
ture is well known in many of the Alge. Mr. Carruthers suggests
that in the arborescent Lessonie we have a near approach to the
Devonian Nematophycus or Prototawites. Many of the stems in
Lessonia measure a foot in diameter and 30 feet in length. The
Laminarie of our own shores exhibit a pseudo-exogenous growth ;
but, as is well known, the difference in growth between the Antarctic
Lessonia and the genus Laminaria consists in the “ exogenous in-
crease in Laminaria being from below upwards, according to the
growth of the roots, while in the genus Lessonia the growth is
from above downwards, in proportion to the increase of the leaves”*.
Macrocystis belongs to the same natural order (Laminariacez), but
possesses a different habit. I may mention also D’Urvillea Harveyi,
Hook., another of the Laminariaces, which possesses a stem-struc-
ture most closely resembling Nematophycus in the vermiform nature
of the cells or tubes, and their irregular semiparallel arrangement.
Dr. Hooker describes and figures this plant in his ‘ Antarctic Voyage,’
vol. 11. t. 165-6 (fig. 2); a figure of the longitudinal structure of the
stem is given on the plate. The Corwen Nematophycus is converted
into amorphous silex. This condition interferes with the microscopic
structure being readily made out, giving apparently false lines across
the tubes or cells; and whether the spiral fibres are inside or out-
side the large tubes, or independent structures outside, I am unable
tosay ; neither can Mr. Newton or myself clearly make out that the
so-called spiral fibres or concentric lines upon the tubes can be re-
solved into minute dots. His figure (fig. 4) is most carefully drawn ;
and one of the tubes containing the globular bodies is also delicately
and similarly lined. Fresh observations may enable us to determine
whether the spiral lines can be resolved into dots or not. The lon-
gitudinal and transverse sections prepared by Mr. Newton show
every feature described by Mr. Carruthers in his paper. The elon-
gated cylindrical cells, of two sizes, appear completely and irregu-
larly interwoven, as Mr. Carruthers well expresses it, into a kind of
* Berkeleys Introduction to COryptogamic Botany, p. 57; Carruthers,
Monthly Microscopical Journal, 1872, pp. 170, 171.
494 H. HICKS ON THE REMAINS OF PLANTS FROM THE
felted mass ; and in the figure of the longitudinal structure of tho
stem in D’Urvillea Harveyr given by Dr. Hooker (loc. cit.) an irre-
gular vermiform interlacing and interweaving of the cells or tubes
is shown, remarkably agreeing with the structure of Mematophycus.
It would be interesting to ascertain if the large round spore-like
bodies (which are here termed Pachytheca or Pachysporangium, fig. 7)
are the sporangia of Vematophycus: the cells which radiate from the
central cavity are certainly filled with round spore-like bodies ar-
ranged in single file, or disposed in such a manner as to be shed from
the periphery or circumference of the body called Pachytheca. This
is manifest in the structure of one of these cut through and shown
under the microscope (fig. 9). The large tubes or cells, constituting the
stem structure, which appear here and there to contain round spore-
like bodies similar to these, do not really do so; they are, I believe, ac-
cidentally scattered here and there, and appear to be within rather
than upon the tubes in the microscopic sections.
On two of Dr. Hicks’s rock specimens there are singular honey-
comb-celled bodies having all the appearance of being coriaceous or
membranous capsular bodies, or sporangia; the outer portion was
definitely composed of either four- or six-sided cells. This sac-like
body may have played some part in the history of Mematophycus.
Under any circumstances they are worthy of notice, and are un-
doubtedly organic.
The plant called Prototaxites by Dr. Dawson, from the Gaspé
beds, of Devonian age, was one of the oldest plants then known; the
previously known oldest plants are mere fragments of woody matter :
these occur with Pachytheca in the Upper Ludlow, of the Ludlow
area; and no older British rocks have, until now, yielded any.
Looking at the probable distribution of a marine flora the plants
composing which were of such magnitude and probably widely
spread over the Devonian sea-bed, we naturally turn to the origin or
source of the Gaspé Devonian species. The presence of Nema-
tophycus in the Denbighshire Grits is proved by these researches of
Dr. Hicks; but no remains of a similar kind have been found
through the higher beds of the Woolhope, Wenlock, and Ludlow
rocks—except at the close of the Ludlow, in the Downton shales,
if the seed-like bodies termed Pachysporangium or Pachytheca are
to be regarded as portions of Nematophycus. If they have no relation
to each other, then we have to account for the wide distribution in
time of both—Nematophycus from the Denbighshire Grits to the
Devonian, and Pachytheca from the Denbighshire Grits to the Upper
Ludiow. We are warranted, I think, in believing that there is far
less chance of these being one species than modified descendants
from an older stock, the entire area never having been dry land at
one time since the deposition of the Denbighshire Grits ; I therefore
give this the specific name NMematophycus Hicks. I look forward
to finding the remains of this group of Algee in rocks of far higher
antiquity ; for it is evident that marine plants of such colossal size
as the Gaspé species is known to have been could not then have
DENBIGHSHIRE GRITS, NEAR CORWEN, NORTH WALES. 495
made their first appearance. Again, the habitat of Nematophycus,
if it at all resembled the present Lessonie in growth at the bottom
of the ocean, may have survived many changes between land and
sea during the deposition of the Upper Silurian rocks, while yet the
sea-bottom or bed of the Silurian Sea was never exposed or became
dry land. The finding and determining the nature of these remains
opens up a great problem, so far as the age, continuity, and distribu-
tion of Cryptogamic life in palzozoic time is concerned.
EXPLANATION OF PLATE XXV.
1. Nematophycus Hicksii: cross section, x 200.
2. Ditto: longitudinal section, x 200.
3. Ditto: tubes filled apparently with granular substance, x 329.
4, Ditto: tubes covered by fine transverse lines, X 320.
5. Ditto: portion of stem, natural size.
6. Ditto: fragments, ditto.
7. Pachytheca: X 6.
8. Ditto: portion of wail, x 200.
9. Ditto: fibre in wail, x 200.
0. Microspores, probably of a Lycopodiaceous plant, x 15.
Discussion.
Mr. Carruruers spoke of the importance of Dr. Hicks’s discovery,
and said that after the President’s note it was needless for him to
add much. He had come in the main to the same conclusion. The
view of the significance of the Pachythece was interesting : but the
data which had come before himself hardly warranted his regarding
them as Algee. He explained the reasons why he was unable to
accept the President’s view, and agreed with that of Sir Joseph
Hooker—namely, regarding them as Lycopodiaceous. He thought
also that the signs of a vascular axis in some of the specimens
proved a land-flora; also there were some spores, not sporangia,
which bore out this view.
Mr. Horpxryson said that the Graptolites were partly Middle
Silurian and partly Upper Silurian forms, some being Llandovery
species, here dying out, and others Wenlock species, first appearing
here. The change in type seemed to imply an alteration in physical
conditions.
Mr. Dr Rance referred to some Ludlow pebbles at the base of the
Carboniferous, and said that anthracite occurred in beds of the Lake-
district of about the same age.
Prof. Duncan spoke of the good fortune which had attended Dr.
Hicks’s investigations in unpromising ground. The cellular plant
discovered by him was a very remarkable one; it reminded him of
Codium. The undulated underpart of the cellulur structure was
very remarkable, indicating a general rugosity ora spiral fibre ; that
fibre occurred in modern water-plants. In one part there was
something like a dissepiment. As in the beds above the Gannister,
there might be a common link here of land- and water-plants. He
496 H. HICKS ON PLANT-REMAINS FROM DENBIGHSHIRE GRITS.
commented on Pachytheca, and asked whether it could have any
relation to the floats in the Sargassum. These old plants seemed
capable of existing under conditions very similar to the present.
Mr. Tawney said he thought a Lepidodendron had been found in
the Silurians of America.
Dr. Hicks said that Saporta had described a species from about
the same horizon, supposed to be a mineralized fern. He thought
that here was an admixture of land- and marine plants, and believed
much more would be found. At. present Nematophycus was the
best. preserved.
Tt. Journ Geol. Soc. Vol. XXXVI. PL. XXVT.
&: S. Yorkshire N. Yorlushire
| Zone of A
A Jia
umstor Bag
chi beds& ioral Fol
Lower Ookie;
| Ouirad Gu |
Passage beds ¢ Rag
{
Oxtard Gru |
a
Fred ‘Dangerfield Lath. 22 Bedtord Street: (overt Garoben WE ;
tw, a od 7 Ler
Quart, Journ Geol. Soc. Vol. XXXVI, PL NXVL.
Derwet:
Piicanee’ tNeMotae) S. Meuse Tegnow Marne. Aube. Laignes Armangon: Youne Lare Bourges. Charentes, Orne Normandy Lays de Bray Botilannais. ¥é v' bore Cron Gunbridge S Yorkshire LN. Yorkshire
R. te. it rR R. St. R. (alter Hebot. ) — Bucks, Lincdnshire v
Tey, Girm
Port,
Beitentean, [Pare]
Portlandia ‘3
: Dara : Zaid,
be L Peerss Gp Bongrisen| 1
: wae ower Bolong rae = : jae
ihr lonian, Oe Rosai Tower Boloniaw — | 2mse |
| ip Tad Fenton Escoall nme ee
gu va A Galera poets hanes lmeapeeeal Vyelen Fryutian
. ipa i ca Freverru Fergutear nao
= cei. ie eee Tileraphie Si] Trpeta ow ieoparpedl
ae i bi Ale felis “[igenretan + = Gvled tre? f a
As Auarcan| | are & lames Us de : bese ia rere} Supracoralline. Die a
[Sirens ae a Deena Bale trl ET e
nase ne = }___—__-} tharly Linwstene as - mt (ike |
seen aes freee es ee Eaweed ey, es Diep
Supra bgaecr] coal |\deor au! line ; ane -——
empose seni re p Orit escrescat a ii 5 ‘
gers ety ss ees a Row ee i
Uke (rt oe atte so aE Fr ;
teres ea aan Be, IBS on ay
ae Orr : fog ane aie) Ce Sas
i ad Ys rereremer f ete Lunesta | J |
Otho d Coit —— a fuliowe L. ————
Orion ay Sie
|
COMPARATIVE SECTIONS ofr UPPER JURASSIC ROCKS, PARIS BASIN ano ENGLAND. Pl et Za Bat Sefer leg
sf cee Ff
f | q My i FRE
; i] ie Gh ae ou Hes
3 Pirie cag, fi
| ¥ i
G } ane ae) ;
at Ue ‘ yas! }
i LOS aaa de
Jab ¥ a Uri
5 f tne
: ; tf b
iv J d ’ 4 ;
4
Fa Mt
Fi f NS CAM Fo)
es
1
A i
» Ly
; ' i eee | i
y pat wie na
eh nN | A ehy
- Besa aes
: i :
— 5 5 a 5
|
fi as a Ae
i oA ; HOME
hehe eS i
: ions
i
1
i ae
eax
d i At re
we sie?
; pain 4!
; :
y
om
‘
rae
tf 1
x
ON THE UPPER JURASSIC OF THE PARIS BASIN. 497
38. On the Corretation of the Upper Jurassic Rocks of ENGLanp
with those of the Contrnent.—Part I. Tar Paris Basry. By
the Rev. J. F. Buaxz, M.A., F.G.8. (Read April 27, 1881.)
[Puarr XXVI.]
In former papers on the Portland Rocks*, the Kimmeridge Clayt,
and the Corallian Rocks +, as developed in our own country, it has
been pointed out that, while the normal deposits of the period
commencing with the Oxford Clay and continuing to the close
of the Jurassic era were essentially argillaceous, the uni-
formity has been broken by certain episodes which have resulted
in the formation of distinct kinds of rocks, but that, in spite of
these episodes, there is a continuousness both in the physical and
biological features, uniting the whole into one great group, to which
the term Upper Jurassic is appropriated. The present study ought
therefore, logically, to include a correlation of the Oxford-Clay series ;
but though the upper portions of that series come to be incidentally
examined, the far wider range and greater constancy of the lower
portion would render its examination a more arduous and _ less
interesting task; and it is found convenient to have for base a
thick mass of clay, which may almost everywhere be recognized,
however much the upper part may be encroached upon lithologically
by the various preludes to the Corallian series. In point of fact,
the rocks hitherto called Corallian in England comprise much that
is placed in the Oxfordian by the French geologists ; and our corre-
lation is therefore only stopped when the rocks universally called
Oxfordian are reached.
The Upper Jurassic rocks of France lie in two distinct areas.
The more northern is that which is drained by the Seine and the
Loire and smaller rivers having a similar direction; the more
southern is a continuation of the Swiss Jura, or lies to the south of
the central plateau of Auvergne. The former constitutes the basin
of Paris, round which city the Jurassic rocks form an irregular
curve; and their development in this range forms the subject of the
present study, the Upper Jurassic rocks of other districts being
left for a future occasion.
Much good work has been done by the French geologists in the
description of the various portions into which this basin may be
divided, and in the correlation of the rocks with one another, by
the aid of which it is possible for a foreigner to pass from spot to
spot, appreciating, confirming, or even correcting the stratigraphical
succession and its interpretation. The advantage that such a
student has is that, instead of being confined to one area, and
being obliged to obtain his ideas from it, he can make the several
* Quart. Journ. Geol. Soc. vol. xxxvi. p. 189.
Tt Op. cit. vol. xxxi. p. 196.
t Op. cit. vol. xxxiii. p. 260.
Q.J.G.S. No. 148. Dh 56
.498 J. F. BLAKE ON THE UPPER
areas mutually throw light on each other, and present a complete
idea of the whole and not merely of isolated fragments. Oppel, in
his work ‘ Der Juraformation, made such a comparative study in
1860; and Hébert, in his pamphlet ‘ Les Mers Anciennes,’ did the
same for the basin of Paris in 1857. Since those dates much new
material has accumulated; and it is possible also to bring English
rocks into the comparison. Hence several fresh questions have arisen,
and divergences of interpretation have been developed, on which
it is impossible to come to any conclusion without a uniform and
comprehensive study in the localities themselves, which will usually
show that nature is much more simple than her various interpre-
ters between them would make her. |
The following numbered list gives some account of what has been
written on the Upper Jurassic rocks of the Paris Basin :—
Inst of Works and Papers consulted on the Upper Jurassic
Rocks of the Paris Basin.
(1) 1825-8. Caumont. Explication de la carte géologique de Normandie. —
(2) 1842. Savvace & Buvienier. Statistique minéralogique et géologique du
département des Ardennes.
(3) 1844. Ravin. Mémoire sur la constitution géologique du Sancerrois.
Bull. Soc. Géol. Fr. ser. 2, vol. it. p. 84.
(4) 1844. Rover. Note sur les terrains jurassiques supérieurs et moyens de la
Haute Marne. Bull. Soc. Géol. Fr. ser. 2, vol. ii. p. 705.
(5) 1844. Royer. Comparaison des terrains jurassiques de l’Yonne avec ceux
de la Haute Marne. Bull Soc. Géol. Fr. ser. 2, vol. 11. p. 714.
(6) 1844. Corrzav, Ann. Stat. de ’Yonne, p. 236.
(7) 1846. Luymertz. Statistique du département de l’Aube.
(8) 1847. Graves. Essai sur la topographie géognostique du département de
VOise.
(9) 1847. Corrrau, Bull. Soc. Sci. Hist. et Nat. de Yonne, t. i. pp. 23 and 367.
(10) 1850. Bounanerr & Bertera. Texte explicatif de la carte géologique
du Cher.
(11) 1851. Royer. Sur quelques failles dans la Haute Marne. Bull. Soc. Géol.
Fr. ser. 2, vol. viil. p. 564.
(12) 1851. Royer. Apergu sur les terrains Corallien et Oxfordien de la Haute
Marne. Bull. Soc. Géol. Fr. ser. 2, vol. viii. p. 600
(13) 1852. Buvienter. Statistique Géologique, Minéralogique, Minérallurgique
et Paléontologique du département cle la Meuse.
(14) 1852. D’Orsieny. Cours élémentaire de Paléontologie et de Géologie stra-
tigraphiques. Vol. 2,
(15) 1853. Ravin. Sur l Oxford Clay du département de l’Yonne. Bull. Soe.
Géol. Fr. ser. 2, vol. x. p. 485.
(16) 1855. Correav. Notice sur lage des couches inférieures et moyennes de
Vétage Corallien du département de ?Yonne. Bull. Soc. Géol. Fr. ser.
2, vol. xii. p. 693.
- (17) 1855. Manis. Statistique géologique de la Charente Inférieure.
(18) 1856. Corrzav. Compte Rendu de la session tenue par la Société Géolo-
gique de France le 7 Septembre a Joinville (Haute Marne).—Compa-
raison des terrains observés par la Société avex ceux du département
de lYonne. Bull. Soc. Sc. Hist. et Nat. Yonne.
(19) 1856. Réunion Extraordinaire de la Société Géol. de France a Joinville.
Bull. Soe. Géol. Fr. ser. 2, vol. xiii. p. 787 (Royer).
(20) 1856. Buvienter. Note sur les calcaires 4 Astartes et l’étage jurassique
supérieur et moyen de la Meuse et de la Haute Marne. Bull. Soe.
Géol. Fr. ser. 2, vol. xiii. p. 843.
JURASSIC OF THE PARIS BASIN. 499
(21) 1857. Huserr. Les Mers anciennes et leur rivages dans le bassin de Paris.
Part I. Terrain Jurassique.
(22) 1857. Buvienter. Observations sur le terrain jurassique de la partie
orientale du bassin de Paris. Bull. Soc. Géol. Fr. ser. 2, vol. xiv. p. 595.
(23) 1858. Coquanp. Description géologique de l’étage Purbeckien dans les
deux Charentes. Bull. Soc. Géol. Fr. ser. 2, vol. xv. p. 577.
(24) 1858. Coquanp. Statistique de la Charente.
(25) on LeymericE & Ravuin. Statistique géologique du département de
*Yonne.
(26) 1858. Réunion extraordinaire de la Société Géologique de France a Nevers
(Ebray). Bull. Soc. Géol. Fr. ser. 2, vol. xv. p. 680.
(27) 1858. Opprt. Die Juraformation.
(28) 1860. Héserr. Du terrain jurassique supérieur sur les cotes de la Manche.
Bull. Soc. Géol. Fr. ser. 2, vol. xvii. p. 300.
(29) 1861. Gousrrr. Note sur le gisement de Glos. [Ina “ Note sur les Tirigonies
clavellées de VOxford Clay et du Coral Rag,” by M. Hébert.|] Journ. de
ae Apr. 1861. See also Bull. Soc. Géol. Fr. ser. 2, vol. xviii.
p. 520.
(30) 1863. Dotirus. La Faune Kimméridienne du Cap de la Héve.
(31) 1863. Hiserr. Observations Géologiques sur quelques points du départe-
ment del’Yonne. Bull. Soc. Sc. Hist. et Nat. Yonne, 1863.
(32) 1864. Esray. Etudes Paléontologiques sur le département de la Niévre.
(38) 1865. Rieavx. Notice stratigraphique sur le Bas-Boulonnais. Bull. Soc.
Acad. Boulogne.
(34) 1865. Corrzav. Deux jours d’excursion dans le terrain jurassique des
environs de Tonnerre (Yonne). Bull. Soc. Sc. Hist. et Nat. Yonne, 1865.
(35) 1865. Waacen. Versuch einer allgemeinen Classification der Schichten des
oberen Jura.
(36) 1866. Punuar. Notes sur les assises supérieures du terrain jurassique de
Boulogne-sur-Mer, &e. Bull. Soe. Géol. Fr. ser. 2, vol. xxiii. p. 193.
(37) 1866. Hipert. Note sur le terrain jurassique du Boulonnais. Bull. Soc.
Géol. Fr. ser. 2, vol. xxiii. p. 216.
(38) 1866. Samann. Observations sur les communications précédentes, 1. ¢.
p. 220.
(39) 1866. Dz Lorton & Petuat. Monographie paléontologique et géologique
de l’étage Portlandien des environs de Boulogne-sur-Mer. Mém. Soc.
Phys. Genéve, tom. xix.
(40) 1867. Tompecx. Note sur Vétage Portlandien de la Haute Marne et son
parallélisme avec celui du Boulonnais. Bull. Soc. Géol. Fr. ser. 2,
vol. xxiv, p. 187.
(41) 1868. Pzuvar. Observations sur quelques assises du terrain jurassique
supérieur du Bas-Boulonnais. Bull. Soc. Géol. Fr. ser. 2, vol. xxv.
p- 196.
(42) 1868. De Lorton & Corrzav. Monographie paléontologique et géologique
de l’étage Portlandien du département de ’Yonne. Bull. Soc. Se. Hist.
et Nat. Yonne, ser. 2, tom. i.
(43) 1868. Corrzav. Nouvelles observations sur le terrain jurassique des en-
virons de Tonnerre. Bull. Soc. Se. Hist. et Nat. Yonne. ser. 2, tom. ii.
(44) 1868. Tompecx. Note sur le terrain Portlandien de la Haute Marne.
Bull. Soc. Géol. Fr. ser. 2, vol. xxv. p. 456.
(45) 1868. Tomsecx. Note sur les terrains Corallien et Kimmeridien de la
Haute Marne. Bull. Soc. Géol. Fr. ser. 2, vol. xxv. p. 458.
(46) 1870. Petar. Sur l’étage Portlandien du Paysde Bray. Bull. Soc. Géol.
Fr, ser. 2, vol. xxvil. p. 683.
(47) 1870. Prewuar. Nouvelles observations sur quelques assises du terrain
jurassique supérieur du Boulonnais. Bull. Soc. Géol. Fr. ser. 2,
vol. xxvii. p. 683.
(48) 1870. Tompeck. Sur les étages jurassiques supérieurs de la Haute Marne.
Bull. Soc. Géol. Fr. ser. 2, vol. xxvii. p. 687.
(49) 1870. Lennier. Etudes Géologiques et Paléontologiques de la Haute
Normandie.
24 2
500 J. F. BLAKE ON THE UPPER
(50) 1872. Dr Lorton, Rover, & Tompzck. Monographie des étages jurassiques
supérieurs de la Haute Marne. Mém. Soc. Linn. Norm. vol. xvi.
(51) 1872. Savvacr. Note sur la position des couches a polypiers et a Terebra-
tula insignis dans le Boulonnais. Bull. Soc. Géol. Fr. ser. 2. vol. xxix.
p. 215.
(52) 1872. Pruiat. Observations en réponse a la communication de M. Sau-
vage sur la position stratigraphique des calcaires du Mont des Boucards.
Ibid. p. 223.
(53) 1873. Ricaux. Notes pour servir ala géologie du Boulonnais. I. Notes sur
quelques sondages. Bull. Soc. Acad. Boulogne.
(54) 1873. Hupert. Note additionelle 4 la communication relative a létage
Tithonique. Bull. Soc. Géol. Fr. ser. 3, vol. i. p. 67.
(55) 1873. Tomerck. Note sur l’Oxfordien et le Corallien de la Haute Marne.
Bull. Soc. Géol. Fr. ser. 3, vol. i. p. 335.
(56) 1874. Dz Lorton & Pettat. Monographie Paléontologique et Géologique
des étages supérieurs de la formation jurassique des environs de Boulogne-
sur-Mer. Parti. Mém. Soc. Phys. Genéve, tom. xxiii. p. 253.
(57) 1874. TomBecx. Note sur l’Oxfordien et le Corallien de la Haute Marne.
Bull. Soe. Géol. Fr. ser. 3, vol. ii. p. 14.
(58) 1874. Tomsrcn. Note sur une excursion géologique faite au travers des
terrains Coralliens et Oxfordiens de la Haute Marne. Bull. Soe. Géol.
Fr. ser. 3, vol. ii. p. 251.
(59) 1874. Bayan. Sur la succession des assises et des faunes dans les terrains
jurassiques supérieurs. Bull. Soc. Géol. Fr. ser. 3, vol. ii. p. 316.
Followed by observations by Tombeck and Pellat. Ibid. p. 348.
(60) 1875. Dovvittx & Jourpy. Note sur la partie moyenne du terrain juras-
sique dans le Berry. Bull. Soc. Géol. Fr. ser. 3, vol. iii. p. 93.
(61) 1876. Dz Lorton & Pettat. Monographie, &e. des ét. sup. jur. de Boulogne.
Part ii. Mém. Soc. Phys. Genéve, tom. xxiv. p. l.
(62) 1876. Putiar. Emersion du sud et de lest du bassin Parisien a la fin dela
période jurassique, et extension de la limite imférieure de l’étage Port-
landien du Boulonnais. Bull. Soe. Géol. Fr. ser. 3, vol. iv. p. 364.
(63) 1876. TripoLer. Sur les terrains jurassiques supérieurs de la Haute
Marne comparés a ceux du Jura suisse et francais. Bull. Soc. Géol. Fr.
ser, 3, vol. iv. p. 259.
(64) 1876. Tompecx. Note sur le Corallien et lArgovien de la Haute Marne.
Bull. Soe. Géol. Fr. ser. 3, vol. iv. p. 162.
(65) 1877. Tompzcx. Coralliende la Haute Marne. Bull. Soc. Géol. Fr. ser. 3,
vol. v. p. 24.
(66) 1878. Toucan Sur la position vraie de la zone 4 Ammonites tenuilobatus
dans la Haute Marne et ailleurs. Bull. Soc. Géol. Fr. ser. 3, vol. vi. p. 6.
(67) 1878. Srruckmann. Der obere Jura der Umgegend von Hannover.
(68) 1878. Prnuat, Résumé d’une description du terrain jurassique supérieur
du Bas Boulonnais, &e.
(69) 1879. Dz Lapparentr. Le Pays de Bray.
(70) 1879. Tomprck. Réponse aux observations de M. Buvignier. Bull. Soc.
Géol. Fr. ser. 3, vol. vi. p. 310.
On studying these writings it soon becomes obvious not only that
questions of theory are in dispute, but that facts are variously
stated also, and that the latter must first be settled before the
former can have a solid foundation. The study therefore becomes
divided into two parts :—first, observations made for the verification
or modification of the accounts of the true sequence in the various
areas ; and, secondly, discussion of the opinions expressed on the
relations and groupings of the rocks, with special reference to the
equivalents in our own country.
Within the area here spoken of as the Paris Basin there are five
ranges, of very unequal size and importance, separated from each
JURASSIC OF THE PARIS BASIN. 501 —
other by intervals in which older or newer rocks occupy the surface
of the ground. ‘These are 3
I. From the Ardennes to the Cher.
JI. The two Charentes.
III. Normandy, with Orne and Sarthe.
IV. The Pays de Bray.
V. The Boulonnais.
The first-named district, though not the nearest to England, nor
presenting characters most similar to those of our own country, yet,
from its large size, the continuousness of its deposits and the labour
that has been bestowed upon them, presents itself as the most typi-
cal for France, and the one therefore to be studied first, so that we
may better understand the last three, which in some sense are in-
termediate between the French and English types.
I. From tHe ARDENNES TO THE CHER.
Although this range has been studied continuously from one end
to the other, it is necessary in description to subdivide it into those
smaller areas which have been made the subjects of special mono-
graphs by French geologists.
1. The Ardennes Depariment.—The rocks of this area have received
illustration at the hands of MM, Sauvage and Buvignier (2)*, who
give the following classification
1. Uprer Group.
a. Marls with Exegyra virgula, 160 ft.
6. Caleaire 4 Astartes, 21 ft.
2. Corau Raa, 250 ft.
3. OXFORDIAN.
a. Ferruginous oolite, 28 ft.
b. Marls and limestones, 300 ft.
(1) Shelly siliceous limestone, (2) marls, (3) ironstone.
e. Lower marls with ironstone, 30 ft.
Commencing this series from the base, 3 ¢ may be passed over as
Callovian, while 3 6 (2) and (3), forming the great mass of the 300 ft.
and occupying the valleys, will represent the undoubted Oxford Clay.
The series 36 (1) then commences the group of rocks now under
study. If for “siliceous limestone” we read its equivalent, ‘“ calca-
reous grit,” we have the term which will exactly suit the English
geologist, who at once recognizes in it a representative of his ‘ Lower
Calcareous Grit.’ At the base, as seen in quarries on the road from
the station of Launois to Neuvizy, is hard blue cale-grit ; and above
this, nodular beds of grit in a subargillaceous matrix. Some of
these are very light, like the Upper Calcareous Grit of Yorkshire, and
are said by Sauvage and Buvignier to be soluble in potash, indicating
a possible organic origin, like the Renulina-grits of Scarborough ;
the fossils, however, are in some cases ‘ beekized.’ These nodular
_ beds, which begin to present some of that peculiar feature indicated
* See list of works above.
502 J. F. BLAKE ON THE UPPER
Fig. 1.—Map of Country near Neuvizy. (Scale 1 : 80,000.)
x L aunots L
by the term ‘terrain a chailles’**, contain a characteristic fauna, viz.
Ammonites cordatus, Modiola bipartita, Perna quadrata, Pecten fi-
brosus, Avicula expansa, Exogyra spiralis, Ostrea dilatata, O. rastellaris
Rhynchonella Thurmanni, and several others less certainly identified,
but all indicating a horizon similar to that of the Nothe grits and
clays or of the Lower Calcareous Grit of Yorkshire. At the top this
series becomes much more calcareous, and finally contains abundant
oolitic grains, while a change of fauna takes place. This has been
very imperfectly examined; but the three chief species are Ammo-
* This term “terrain a chailles” is a misleading one. It is often used as if
indicating a fixed horizon ; but it appears from French writers that there is one
of these ‘terrains’ in the Callovian, another in the Oxfordian (the present
one), and a third in the Corallian ; so that it is really a mere petrological phrase
similar to “nodular beds”.
JURASSIC OF THE PARIS BASIN. 503
nites oculatus of the variety called A. Bachianus, Oppel, Trigonia
spinitfera, d’ Orb. (Prodr.), and Rhynchonella Thurmanni. The Tri-
gonea is specially noticeable: it has been found by Mr. Hudleston at
Snainton in Yorkshire, in a quarry belonging to the passage beds
above the Lower Calcareous Grit, and named by Dr. Lycett 7’. snain-
tonensis ; but, though never figured by the French geologists, it seems
to be abundant in the Ardennes department, and occurs on the same
horizon in the Vosges. The Ammonite serves to show how essen-
tially Oxfordian these beds still are. Their total thickness is about
50 feet.
Next in the series is the Ferruginous Oolite, which, from its easily
recognized mineral character and its rich fauna, has attracted con-
siderable attention, and has been constantly used by authors as a
term of comparison for beds in other districts. It is of no great
thickness, 28 feet being given asitsmaximum. At Vieil-St.-Remy it
is an earthy limestone with scattered oolitic grains of limonite and
crowded with fossils.
At Neuvizy almost every thing but the oolite grains has been dis-
solved, and these remain as a loose deposit containing ‘ beekized’
fossils with vacuous interiors. The latter character, however, is
exceptional, as the bed may be traced in the former character as far
south as Commercy, if not further, a distance of 100 miles. It is,
in fact, remarkable for its constancy, especially as compared with the
beds above it; and if a division is to be made in the series in this
district on stratigraphical grounds, it is certainly over this that
the line must be drawn. From this rock more than 200 species
have been recorded in this department, and 190 in the department
of the Meuse. In such a fauna one naturally finds representatives
of species which are abundant on several horizons; and one may
therefore easily be misled to place it on any horizon that one hap-
pens to be most familiar with. Two Ammonites are common, Viz.
A. cordatus and A. Martelli, the latter being the A. plicatilis of
dOrbigny. A form which may belong to the true A. plicatilis occurs
in the same beds in the Meuse department ; and d’Orbigny and Buvig-
nier both quote A. perarmatus from this horizon as well as from the
beds below. Amongst the Gasteropoda quoted from here, Cerithium
muricatum, Littorina muricata, Pseudomelania striata, Chemnitzra
heddingtonensis and Bulla elongata are constantly met with in the
lower Corallian limestones in England, the Pseudomelania being
more characteristic of higher beds. Amongst the Lamellibranchiata,
Gryphea gigantea, Pecten fibrosus, Lima gibbosa, Gervillia aviculo-
ades, Avicula ca:pansa, A. ovalis, A. polyodonta (the same as our
A. pteropernordes), Perna quadrata, Mytilus pectinatus, Cucullea
oblonga, Opis similis, Astarte extensa, Tancredia curtansata, Iso-
donta Deshayesia, Myacites decurtatus, and Pholadomya ovals are
most noticeable as confirming the evidence of the Gasteropoda ; but
Peeten vimineus points to arather higher horizon; while the presence
of Rhynchonella Thurmanni, and of what is probably R. lacunosa, with
abundance of Waldheimia buceulenta and Terebratula fileyensis, is
still in harmony; and finally the echinoderms Willericrinus echinatus,
504 J. F, BLAKE ON THE UPPER
Echinobrissus scutatus, Holectypus depressus, and Collyrites bicordatus
add their testimony to the great similarity which the fauna of this
ironstone bears to the lower portions especially of the calcareous
series of our Corallian rocks.
This Ferruginous Oolite is referred by Hébert (21) to the middle
Oxfordian on the ground that above it at Vieil-St.-Remy occurs a
great thickness, 160 feet, of brown marls with a thoroughly Oxfordian
fauna, such as Ammonites arduennensis, Trigonia perlata, Gervillia
aviculoides, Ostrea dilatata, &e. The occurrence of any such marls is
denied by Buvigner (22) who states that the Oolite seen below must
be out of place. Certainly no such thickness of marl was observed
where the beds were examined. About 40 feet of marls are seen at
the base of the valley near Vieil-St.-Remy and in the railway-cut-
ting near Neuvizy ; but these, from their position, are more probably
below the Ferruginous Oolite, which is seen too near to the Corallian
limestones on the road between Vieil-St.-Remy and Novion to allow
of any intervening clay of more than a few feet thickness. It is
probable therefore that the Grit and Ferruginous Oolite are hidden
on the road to Wagnon in the 160 feet, the base of which contains the
above fossils, while over it come the marly limestones recorded to
contain Cidaris florigemma and Pecten articulatus. In many other
places further south also some representative of the Coral Rag is
found immediately overlying the Ferruginous Oolite ; so that its posi-
tion is, in reality, perfectly fixed.
The constancy of this bed in spite of its thinness is in striking
contrast with the variability of the succeeding series on the horizon
of the T'rzgonia-beds of Pickering or of the earliest limestones of the
Corallian series, which are said by Buvignier to have nothing constant
but their inconstancy.
In the neighbourhood of Vieil-St.-Remy and Neuvizy the lowest
beds referred to the Coral Rag are not well seen, though Hébert (21)
describes about 4 feet to 5 feet of coral material with Cidaris forigemma
on the road to Wagnon. Nowhere here, however, is there any great
thickness of such growth ; and what there is is succeeded immediately
by the white limestone which is seen so well at the quarries of No-
vion. This limestone has been much acted on by chemical agents,
many of the fossils being silicified and others represented only by
casts. Among the latter the corals are of the greatest importance ;
the majority are not Thamnastreean but Calamophyllian and Clado-
phyllian. MM. Sauvage and Buvignier simply place the whole of
these limestones, amounting, according to their estimate, to 250 feet, as
Coral Rag, without further subdivision, and supply a rather defective
list of fossils. At Novion a magnificent section, 100 feet in thickness,
is seen, the Calamophyllic in places almost forming a reef at the
base; then follow great false-bedded masses of fine white limestone,
and towards the top huge crystalline nodules of Thamnastree.
Lithologically therefore this might well pass as a Coral Rag; and it
represents in this area all that would naturally be called Corallian.
When, however, we examine it more closely, we note in the first
place that this is scarcely a Thamnastrean reef, such as is usual in our
JURASSIC OF THE PARIS BASIN. 505
true English Coral Rag, the specimens at the top not being in situ—
and also that there is an apparent absence or great rarity of Cidaris
florigemma, the spines which occur being either smooth or belonging
to C. Smith. At the base the most abundant fossil is a large
Natica like N. millepunctata, Buv., but perhaps WV. grandis; while
the topmost beds are crowded with silicified Nerinew, NV. sequana
bring the most abundant. Other noteworthy fossils are rarer ex-
amples of Diceras arietinum?, Cardium corallinum, Cerithium lime-
forme, Pteroceras oceani (undistinguishable from those at Boulogne),
Lima equilatera, Buv., and L. ornata, the Modiola wmbricata, Rom.
(non Sow.), and Zerebratula. MM. Sauvage and Buvignier mention
also among others Arca pectinata, Pecten articulatus, and Chemmitzra
heddingtonensis. These characters taken together appear to indicate
a higher horizon than the ‘ floregemma’ Rag, namely one which in
spite of its abundant corals should be paralleled with Supracoralline
beds elsewhere, or the upper part of theCorallian series when that has
been divided as it has been in the Meuse. The upward succession
is not well seen in this neighbourhood, the great limestones passing
to large-grained oolites with undistinguishable fossils, and then to
more compact limestones referred to the Astartian.
The interpretation of the rocks seen in this district may now he
checked by an examination of the country about 20 miles distant to
the south. Starting from the town of Beaumont, and going westward,
after passing over the Lower Oolites, the Kelloway hock and the
Oxford Clay, which is here well developed in an argillaceous form,
one comes, at the base of the escarpment of Stonne, to the same sandy
nodular beds with Rhynchonella Thurmanni and Perna quadrata as at
Neuyizy,. duly followed on the top of the hill by the Ferruginous Oolite ;
but the bed with Trigomia spinifera was not observed. Above this,
on the road to Ochsee, a village three miles south, the succession
is perfectly observable on the rough cart-road mounting a barren
hill; at the base are the Lower Calcareous Grit and the Ferruginous
Oolite ; near the sammit are the great cavitary limestones of Novion,
where the Calamophyllie have been, and above them flaggy Oolites
&e. full of Nerinee ; but in the intervening space there is no sign of
clay, all is calcareous. This portion, however, contains abundant
Thamnastrean corals ; and with them Cidaris florigemma was easily
found associated with Hemicidaris crenularis, Cerithium muricatum,
and Littorina muricata ; but the Nerinee and Natice of the limestone
above are absent. It thus appears that we are justified in regarding
the Novion limestone as Supracoralline; while al] that can represent
the series so well developed in England between the Lower and the
Upper Caleareous Grit is the Ferruginous Oolite and the Rag Lime-
stone. The upper portions of the series have not been examined
in the Ardennes department, as the description given by the before-
named authors indicated that they were similar to those to be seen
in the northern part of the Meuse.
2. The Meuse Depariment.—On entering this we come under the
guidance of Buvignier alone (13), whose classical work is well known.
He gives the following classification.
506 J. F. BLAKE ON THE UPPER
1. Upper JuRASSIC.
I. Barrois limestone, 600 feet.
a. Grey-green limestone.
6. Carious limestones.
¢, Lithographic limestones,
II. Virgulian clays, 150 feet.
III. Astartian limestones, 400 feet.
a. Upper compact limestones.
6. Lower marls.
2. Mripp1E JurRAssIc,
I. Coral Rag, 400 feet.
a. Lithographic limestones.
6. Various forms.
II. Oxford clay, 500 feet.
a. Ferruginous oolite.
6. Siliceous limestones=Terrain 4 chailles.
c. Woévre clay.
Near the northern extremity of the department, in the neighbour-
hood of Dun, the lower portions of the series may be easily taken
up again; and they show a continuance of the conditions last noted
in the Ardennes. On the slopes of the Cote St. Germain a fairly com-
plete section may be seen: the lower half is occupied by the Oxford
Clay, with the topmost part of the same nodular gritty character as
before ; then may be seen the Ferruginous Oolite, of some thickness ;
immediately over which come great crystalline irregular masses
which, in spite of their present state, are easily recognized as remains
of a Thamnastrean reef, with which Cidaris florigemma occurs ;
this portion is also considerably oolitic, differing in this respect from
the limestone that follows it, which, with its vacuous spaces once
filled with corals and Nerineew, perfectiy represents the Novion
stone. Here, then, we find confirmation of previous sections. Hébert
(21) states that the Coral Rag alone is seen at the base of this hill-
side, and that the Ferruginous Oolite must be some distance below,
and separated by a great mass of clay. The sequence, however, is
here perfectly clear; and on the opposite side of the valley, in the hill
between Murvaux and Fontaines, the same succession is equally well
seen. Only at this spot the true Coral Rag has greatly developed, as
may be seen also by its examination in other places in the neighbour-
hood. ‘Thus the great quarries to the south of Dun show perhaps as
much as 60 feet, consisting of a lumachelle of broken shells at the base,
a Thamnastrean reef with Ostrea solitarca in the middle, and oolite
beds with Cidaris florigemma at the top, all of which must be about
on this horizon, and which give an idea of the variability of the
series ; while in the valley leading to Fontaines the still coral-bearing
upper limestones are largely developed, but without the character-
istic urchin of the lower reefs and their equivalents.
Passing next to Verdun, the student who has traced the lower
507
JURASSIC OF THE PARIS BASIN.
= ————
Prazncsezre
Fig. 2.—Map of the Country round Verdun.
i
Se
(Scale 1: 160,000.)
ee
Tater, Verdun Coté
Ae oO ee bi
208 J. F. BLAKE ON THE UPPER
rocks so far has no difficulty in assigning to their true place the
magnificent limestones which here astonish him and give him an
idea of the grandeur of the development of the Corallian rocks in this
district. The beds which in this locality overlie the Ferruginous
Oolite are altogether different from any thing seen before, consisting
at Haudainville of an unstratified mass of limestone 40 feet in thick-
ness, made almost entirely of fragments of crinoids united by a cal-
careous cement and yet distinct, forming a most admirable freestone :
the only fossils seen in it are Cidaris florigemma and small oysters.
Capping this mass in the quarry is 10 or 12 feet of Thamnastrean
Rag with occasional Cladophyllic, but with abundance of Cidaris
florigemma, Terebratula maltonensis, and Pecten vimineus, also Lima
leviuscula and Venerwpis corallensis. 'The position, then, in this
locality of the crinoid limestone is fixed; for it must be associated
with the Rag above it, as forming part of Buvignier’s Coral Rag 0.
The succeeding rocks, representing the Novion limestones, also intro-
duce new features ; for here is first seen the lithographic stone which
becomes so abundant further west. It is mixed with Oolites of
various-sized grains; but the corals of all kinds are gone. ‘The ap-
pearance of this group in the great quarries of St. Martin has been
admirably described by Buvignier—its cherty bands, its vegetable
remains towards the base, and crustaceans above. ‘The fossils are
only abundantin parts: the commonest is Nerinea elongata, associated.
with others, as V. Jollyana and Patella elegans; Natica globosa and
Lucina mosensis were also collected. The upper part of this group
is instructively seen on the north of Verdun, in the Cote St. Michel.
The eastern portion is worked in pure lithographic limestone without
a fossil; but the western shows great quarries of massive earthy lime-
stones in which the characteristic fossil is Terebratula repelimana,
d’Orb., as at Novion, but which shows its relation to the overlying
rocks by its numerous Astarte suwpracorallina, &c. The long lists of
fossils given by Buvignier as coming from his two divisions of the
Coral Rag, of which the present is his a, contain many species in
common, especially Diceras arietinum ; nevertheless there can be little
doubt of their corresponding with beds showing more distinctness
further north. We find therefore the same subdivision of rocks, here
referred to the Corallian, as in the Ardennes,namely a variable mass of
coral-bearing or crinoidal limestone below, with Cidaris florigemma,
and a more compact and oolitic stone above, with many Nerinee,
and an occasional Diceras. Hébert (21) thinks to divide the lower
part into two portions, the base a shell-bed with Cidaris florigemma
and the corals above; but the extreme variability of these rocks, and
the occurrence of the characteristic urchin throughout all the modi-
fications, render such a division valueless.
In this neighbourhood the first examination of the higher: beds
has been made along the road leading from Verdun westwards to
Clermont-en-Argonne. Leaving the town by the fort on the north-
west, one’s position is accurately determined by observing the great
coral-reefs on which the foundations are built, associated with the
gasteropod-bearing intercoralline brash, followed in the railway-cut-
JURASSIC OF THE PARIS BASIN. 509
ting by the massive rocks of the Nerinzan series as seen on the
opposite side of the river. Succeeding these at once are more marly
rocks than any seen before ; in fact they are alternations of marls and
flagey earthy limestones, with here and there a bed of oolitic rock,
a lumachelle of Exvogyra bruntutana, or alithographic limestone. The
thin beds having their surfaces crowded with Astarte supracorallina,
indicate with certainty the horizon. Rocks of this description occupy
the country for a distance of five miles, till the lowest Virgulian
lumachelle is reached, and seem tobe rather uninteresting and barren.
Nevertheless Buvignier describes the lithographic stones as massive,
and overlain by an irregular pisolite having the fossils as casts, in-
cluding Diceras and Cardium Buvigniert, a species which appears to
be not different from C. corallinum. This would seem to indicate a
repetition of the Diceras-beds at a higher horizon than the first, namely
immediately beneath the Virgulian; and the list of fossils givenasfrom
the upper portion of the Astartian limestones contains several species
usually of a lower horizon, such as Lima equilatera, Pecten articula-
tus, Chemnitzia heddingtonensis, Natica globosa, &c. These pisolites
are said to occur in the very district now under notice ; but though
the various sections were duly searched, no such rock was observed
in the required position. At Baleycourt quarries were seen in which
the stone was very rubbly ; but it had the aspect entirely of a rede-
posited material with the fossils in it remanié, and not at all like the
true Diceras-beds of the Haute-Marne. With this exception, no
change in the character of the rocks is observable till the lumachelles
with Exogyra virgula are reached. If therefore any portion repre-
senting the Pterocerian beds is to be found, it must be sought either
in the beds containing #. virgula or in the lithographic limestones
below. The latter are credited with an enormous thickness (400 feet),
and obviously include much more than is usually placed in the
Astartian beds. In point of fact, there seems little to characterize
the beds here; and their subdivisions must be left somewhat
doubtful.
In the Virgulian marls which follow wehave fortunately an admir-
able landmark, both because the abundance of the little oysters (which
in themselves make half the bed) renders these marls immediately
recognizable, and because the variety of their other fossils gives
good materials for correlation. At the cutting of Nixéville the dark
~ marls with Z. virgula occupy the lower 12 feet, and white chalky
limestones the upper 20 feet ; neither therefore is seen in its full
thickness. For a considerable distance to the west, alternations of
these two forms recur, the marls being the last seen beneath the
overlying lithographic limestone. The whole series does not appear
to occupy so great a thickness as the lower Astartian beds. The white
limestones are extremely fossiliferous, the most abundant shells being
Pleuromya V olizu, Pholadomya acuticosta, Cucullea texta, and Terebra-
tula bisuffarcinata. The other fossils observed were Péerocera Pont,
Chenopus musca, Chemnitzia gigantea, Thracia lata, Mactromya ru-
gosa,Ceromya eaxcentrica, Cardium Bannesianum?, Trigoma Merian
T. Juddu, Pinna granulata, and Nucula Menkei and Astarte swpra-
510 J. F. BLAKE ON THE UPPER
corallina. In spite of the last-named, which is thus seen to have
rather a wide range, the fauna is essentially Lower Kimmeridgian,
and may be well matched in the body of that clay in England. For
purposes of comparison in the basin of Paris itself, the Terebratula,
Pholadomya, and Ceromya should be especially noted. Fragments
of coronate Ammonites which might belong to A. gigas, recorded by
Buvignier, were seen; and it may be noted that A. longispinus is
mentioned as occurring; but there is nothing except the first-named
to unite this to the Upper Kimmeridge of England. Hence, therefore,
there is no probability of the overlying rocks being of Portland age,
as they are called by Buvignier.
In this locality the rocks which succeed the Virgulian beds at
Dombasle are barren, lithographic, but somewhat argillaceous lime-
stones, in remarkably uniform beds of from 8 to 12 inches thickness,
with thin bands of intervening clay, thus presenting a well-marked
lithological character by which they may be distinguished from the
lower lithographic limestones. They become more rubbly towards
the top, but, except for lumachelles of small oysters of unknown
species, contain scarcely a single fossil. They occupy a considerable
area, and must be nearly 100 feet thick; but even Buvignier only
records four fossils :—Ammonites gigas, Pleuromya Voltzw, Cardium
Dufrenoycum, and Patella suprajurensis. Nothing higher is to be
seen in this part of the country, as the lithographic limestones ex-
tend to the alluvial plain separating the Jurassic area from the
cretaceous escarpment.
We may next examine the country 25 miles further south from
St. Mihiel and Commercy to Bar-le-Duc. The first-named is celebrated
for the magnificent fauna of its Rag-deposits, and has been described
separately by Buvignier. The escarpment begins about five miles
to the west of the town, as at Apremont; but inliers close at hand
enable us to recognize the Calcareous Grit, here still more nodular,
with Rhynchonella Thurmanmi and Ostrea dilatata, and the overlying
Ferruginous Oolite, retaining the same characters that it has further
north. But the limestones which succeed these have a much more
extensive development. At the grand section exposed on the de-
scent to Apremont, the actual base is not seen ; but the rubbly un-
stratified mass appears to begin at once. It is here full of unrecog-
nizable Thamnastreean corals (which appear to have been rolled), and
abundance of Hemicidaris crenularis, Cidaris florigemma, Aprocrinus
Rossyanus, Terebratula maltonensis, and Pecten vimineus. There is
a thickness of about 120 feet, all made of similar material except
near the top, where about 16 feet is made of massive crinoidal lime-
stone as near Verdun. ‘This latter type, therefore, as there, is sub-
ordinate to the Coral Rag; and we hence learn the age of the magni-
ficent freestones of this character worked about seven miles to the
south at Lerouville, where the quarries have a 100-foot face, all of
the same material, with occasional Cidaris florigemma, Terebratula
insignis, and other fossils. We note also that, whereas near Verdun
the coral-beds formed the capping to the crinoidal limestones, here
the latter lie at the top or nearly so, and no definite position in the
511
JURASSIC OF THE PARIS BASIN.
(3) =
Chau vor cour€ psy aX
Fig. 3.—Map of Country around St. Mihiel. (Scale 1 ; 80,000.)
= ————_
wes lore,
2 ee
pepe
--
(lor: Coble,
LY ' ‘+, F, BLAKE ON THE UPPER
Coral Rag can be assigned to either of these forms. Above the Coral
Rag, on the road to St. Mihiel, are the more compact, almost litho-
graphic limestones with Nerinee as before, occupying a wide expanse
of country. So far, therefore, the Verdun form is fairly continued ;
but when we examine the exposures seen in other valleys an inter-
esting modification is observed. The deeper sections on the right
bank of the Meuse show the base of the Coral Rag to be occupied
by far more oolitic and regularly-bedded stone than any seen at
Apremont; but on the left bank, quite close to St. Mihiel, a recent cut-
ting gives a first real indication of something corresponding to our true
Coralline Oolite. At the base of this cutting is 8 feet of Ferruginous
Oolite crammed with fossilk—Ammonites convolutus 2, Pholadomya
decemcostata and P. deltoidea, Mytilus pectinatus, Perna quadrata,
Pecten articulatus, Ostrea dilatata, Rhynchonella lacunosa, Terebratula
bucculenta, Collyrites becordatus, Dysaster ovals, and others. Next
comes more than 6 feet of a rather sandy limestone, not exactly
oolitic, but thick-bedded, in which no Cidaris florigemma or
Pecten vimineus could be found, but such fossils as Ammoniies pli-
catilis, Pseudomelania striata, Pholadomya deltoidea, Holectypus de-
pressus, and Stomechinus sp. abound. ‘This mass is equally distin-
euishable from the Ferruginous Oolite and from the Coral Rag, and
occupies the place, hitherto unrepresented, of those deposits which
in England form a basis for the latter. The thickness of this mass
is not well seen here, and is comparatively unimportant ; but at
Creué, 8 miles N.E. from here, Buvignier has described some ‘‘ lower
white limestones ” occupying the same position, 250 feet in thickness ;
and the same occur also to the south of Apremont at Liouville, and
are therefore more or less alternative with the Rag, the great thick-
ness of which may be due to its filling up the hollows between the
lenticular masses of the ‘“ coralline oolite” below. These limestones
contain a fauna very distinct from that of the Coral Rag: urchins are
almost absent ; Myacide abound ; and the whole assemblage is much
more like that in the Ferruginous Oolite, A. plicatilis being the most
abundant cephalopod. It differs, however, from the fauna of the
latter rock in the absence of the characteristic urchins, crinoids,
brachiopoda, and belemnites. In Buvignier’s list 15 of its fossils
are common to the Coral Rag, and 34 to the Ferruginous Oolite ;
but the latter is only 18 per cent. of the number found in both,
so that by any method of percentages these limestones should be
reckoned distinct.
Above the section already referred to, on the left bank of the
Meuse, are about 80 feet of Coral Rag, most massive below, with old
Thamnastree above, and containing all the usual fossils ; and on the
ascent of the hill comes on at once a great thickness of beautiful
pure white oolite containing scarcely a fossil, though a Corbis and.
Diceras were noted ; all this, therefore, only continues what has been
seen before. What lies above has not been seen; but detailed ac-
counts of it asexposed in the cuttings between Lérouville and Loxé-
ville are given by Hébert (21). At Vadonville is seen at the base
a great mass of white limestones, finely oolitic, but in places almost
JURASSIC OF THE PARIS BASIN. les
pisolitic, stated to be 300 feet in thickness *; and above them occur
150 feet ofoolitic beds with various-sized grains, some pisolites,nodules,
and many specimens of Diceras. The whole of this mass is considered
by Prof. Hébert to be above the white limestones of Novion and
Verdun, which would place them in the Astartian of Buvignier, but
that he considers them to be absolutely wanting to the north of St.
Mihiel. From their position in relation to the great crinoidal
limestones of Lérouville, however, not 1800 yards away, their lower
portion can be nothing else than the Novion limestone; and we
jearn that at this spot the peculiar pisolitic character of the Diceras-
beds begins to be observable in this portion of the series towards the
top. Itis remarkable that no mention is made of this in Buvignier’s
work, though the spot is coloured as Corallian. The next cutting,
27 miles te the west, is also described by Prof. Hébert. Here the
base is occupied by the same pisolitic Diceras-beds, their continuance
being accounted for by some folds and reversed dips observed. This
bed is declared by Buvignier (22) to be distinct from that at Vadon-
ville, and to belong to the pisolites he has described from the Astar-
tian. His description, however, of the cuttingsis by no means clear
(13), while Hébert’s is precise and definite. Above these pisolitic beds
come a few feet of oolites, and then a mass of non-oolitic marly
limestone with conglomerates and Ostrea deltoidea. The same series
of cuttings reveal Virgulian beds further to the east at Loxéville,
with many fossils common to the Astartian beds, and, finally, the
lithographic “ Portland ” + limestones (see 21). This is well-deve-
loped in the neighbourhood of Bar-le-Duc, forming the main mass of
the hills. The carious limestones above are well-marked, with their
hollow tubes filled with a brown earth. This is supposed by Tom-
beck to be the original material, and the limestone to have formed
afterwards ; but this can scarcely be the case, as there are in this dis-
trict many fossils in the limestone with their interiors formed of the
matrix but the shell gone. The assemblage of these appears to in-
dicate very shallow-water conditions, as though here one were at the
natural boundary of the deposit; they are mostly small and simple.
Those found are Alaria dionysea, Mactromya rugosa, Plectomya
rugosa, Lucina aspernata, Corbicella Morcana, Lithodomus vietus,
and Cardium pesolinum?. We have very little assistance here to-
wards correlation with our English rocks, and none towards placing
these on a level with the Portland Limestone.
The highest beds seen here are a variable series of rather dirty-
coloured stones with sands &c.; but one remarkable rock requires
special notice. It is the ‘‘ vacuolar oolite,” in which, so to speak,
there are no oolitic granules, though once there were; each granule
has been dissolved, the intervening matrix alone remaining to form
a spongy rock. This becomes in places almost a lumachelle of Corbula
- * The thicknesses given by Prof. Hébert are always very large when estimated,
and require to be somewhat reduced to bring them into comparison with the
estimates of other geologists.
+ The names used by the describers are adopted until the amended nomencla-
ture is proposed at the end of this paper.
mes. G.S. No. 148. 2u
514 J. F. BLAKE ON THE UPPER
mosensis ; and the next abundant shell is Astarte rugosa. Buvignier
records also Trigona gibbosa, but with doubt. These beds may very
well represent the true Portland Limestone, which is also character-
ized by Astarte rugosa; but this question will be decided later on.
One more traverse completes
Fig. 4.—Map of Country be- ourstudy of the Meuse department.
tween the Meuse and Ornaim. This is about 25 miles to the
(Scale 1 : 80,000.) south, but runs N.W. to 8.E.,
7 the general trend of the strata
changing near the extremity of
the department to be N.E. and
S.W. instead of N. and 8. The
whole series spreads about 84
miles on either side of Gondre-
court, actually commencing within
the Vosges department.
The lowest beds are exposed
at Greux, on the Meuse; and we
still see the nodular calcareous
grits at the top of the Oxford Clay,
here more approaching what could
be called a “ terrain-a-chailles ”
than anywhere else, and still cha-
racterized by Lthynchonella Thur-
manni. No sign, however, of the
== 7. 6 | Ferruginous Oolite was observed ;
=e OU | a vac Buvignier does not place it
eae See) here on his map. It has therefore
: probably died out; for it is not
seen again to the west. Neither is
any thing like the Creué Limestone
or “Coralline Oolite” seen; but
the great mass of Coral Rag im-
mediately succeeds. This consists
of a rubbly rock, in places oolitic,
without any corals, yet of that pe-
culiar appearance which indicates
the beds associated with them;
= tase and all the usual fossils abound,
ae SS (Liecers such as Cidaris florigemma, Hemi-
= Zeomest) cidaris crenularis, Mytilus angula-
= a tus (jurensis), &c. It is succeeded
SS iN He nay f (Cigrky by a white chalky limestone with
| aa \e deine Ok Lemes numerous hollow branches as of
| Xd = Cora ie: d decayed corals, such as are seen
== ; at Novion. Some beds are flaggy ;
PALL. \. but all very barren of fossils.
Greual | f Above comes 12 feet of strong beds
’
Kay
‘ A
Domremy 3. \ Likleey g
of oolitic and non-oolitic limestones,
which are worked for building-
JURASSIC OF THE PARIS BASIN. 515
stone when thickened out in the neighbourhood; and, finally, coarse-
grained thin-splitting oolites occupy the summit of the hill. There
is thus no proof of our having here reached the top of the limestones ;
and yet these are at least 300 feet above the Oxford Grit, all of
which must be placed in the Coral Rag and Supracoralline beds.
The continuation of the route, however, reads us a very instructive
lesson. On consulting Buvignier’s detailed map it will be seen that
behind this hill there is a long tongue of the lower rocks crossing
the road in the valley. Little is to be seen on the descent of the
hill; but on the next rise at Vouthon Bas, the nodular Oxford Grit
is seen in the village, and above this successively a shelly limestone
full of Cidaris florigemma, massive oolitic rocks, thin-bedded oolitic
rocks, and then the lithographic lmestone—in a word the same
succession as before, but in this instance crowded into a space which
certainly cannot exceed 50 feet. So great a change in thickness in a
distance of less than 3 miles gives an idea of the very local and
fragmentary character of the Corallian rocks.
The greater part of the distance to Gondrecourt, about 5 miles,
is occupied by compact, almost lithographic limestones, with no
fossils visible. ‘These appear to be placed by Buvignier, from the
colouring of his map, as Astartian. They nevertheless occupy the
position of the great masses to the north of Verdun, and perhaps
also east of St. Mihiel, which are coloured Corallian; but in the
absence of fossils it is difficult to say to which they should be joined.
In this traverse, as in the others, but little sign is seen of the piso-
litic Diceras-beds ; only some coarse-grained oolites are seen. Hence
the peculiar character so well seen further west is here only occa-
sional, or occupies too small a space to be easily discovered.
Near the entrance to Gondrecourt these lithographic limestones
are succeeded by and intermixed with rubbly beds with many
fossils. A thickness of about 40 feet is seen, towards the top of
which Terebratula subsella is abundant. Similar stone is continued
for nearly a mile on the other side of Gondrecourt, and gives a very
good idea of the Astartian beds in this district. The fossils here
noted were Terebratula sp. (perhaps the young of 7’. subsella),
Pterocera Thirrie, Thraca lata, Pholadomya Prote, Isocardia obovata,
Ceromya excentrica, Pleuromya rugosa, Mytilus opisoides?, and
Nautilus inflatus. Exogyra virgula is not seen in these beds, which
are almost as argillaceous as the overlying series, especially if we
include in them all that lies below the first undoubtedly Virgu-
lian bed; but no pisolitic beds are seen along the road. The base
of the Virgulian occurs at Houdelaincourt, about 3 miles north of
Gondrecourt, where a mass of chalky limestones forms a bank 40 feet
in height, the upper part of which yields all the fauna of Nixéville, e.g.
Ammomtes longispinus, Pholadomya multicostata, P. Prote:?, Astarte
supracorallina, Pinna granulata, and Pecten suprajurensis. Above this
come the marls full of Hvogyra virgula, then more chalky lime-
stones with Pleuromya Voltzi, and finally more marls and marly
limestones such as are seen in a cutting further on. This cutting,
made for the Marne-and-Rhine canal at Demanges, has been de-
2M 2
516 J. F, BLAKE ON THE UPPER
scribed and drawn by Buvignier. It shows well how argillaceous the
Kimmeridgian is here, being composed of quite as much clay as stone,
which is an exception to its usual character in France. About 40 ft.
is exposed; but this does not include any lumachelles of Haogyra
virgula, though that oyster occurs with others. The nodular bands
are very fossiliferous, and include more stony beds at the base, with
Pholadomya multcostata, Gervilha kimmeridiensis, and Cucullea
texta, and in more marly beds . terocera mosensis, Trigonia Voltzi,
T. concentrica, Astarte scalaris?, Pleuromya Voltzu, P. donacina ?,
Pecten suprajurensis, and Terebratula subsella.
This description of the beds which intervene between the Corallian
and ‘‘ Portland” limestones, though doubtless indicating that some
division might be adopted, does not tend to magnify the importance,
in this district at least, of the three groups—Astartian, Pterocerian,
and Virgulian, all of which would be included in England in the body
of the Lower Kimmeridge. There is a community of fauna which
shows them all to be too intimately united for any wide separation.
Above the fossiliferous Virgulian marls of the Demanges cutting
comes immediately the unfossiliferous lithographic limestone of the
so-called “‘ Portland” series, occupying all the summits of the hills;
but no special observations were here made.
3. The Haute-Marne Depariment.—The development of the Upper
Jurassic rocks in this department has received more study and raised
more discussions than that in any other place. It is consequently con-
sidered by many the typical region in the Paris basin, and is used as
a term of comparison in every attempt at correlation. Lying opposite
the strait which connects the basin of Paris with the Jura, its lower
part appears to partake of the character of the Swiss rocks ; and its
upper part is more complete than anywhere else in the same range.
Although it is therefore of the highest importance that its rocks
should be correctly described and interpreted, the difficulties of its
natural situation appear to have been increased by its illustrators,
and one would suppose from their writings that it was of most ano-
malous structure. The earliest description was given by Royer (4).
Being the simplest, this was in some respects the best; and it will
be well to quote it for comparison with the most recent and com-
plicated. Royer divides the series as follows :—
A. Portland. Oo.iTE or BaRrols.
a. Carious limestones.
6. Nodular compact limestones.
c. Lithographic limestones.
. Kimmeridgian.
. Astartian.
a. Nodular and oolitic beds.
b. Compact limestone.
. Coralline oolite.
. Compact Corallian limestone.
a. Thick limestone.
b. Marly limestones passing to Oxfordian ; 6’. Rubbly coral limestone.
. Upper Oxfordian marls, almost without fossils.
. Middle Oxfordian.
. Lower Oxfordian.
Eo Qh
FY C2 te
JURASSIC OF THE PARIS BASIN. 7
Various changes have since been made in this classification, partly
by way of expansion, but partly by way of alteration; and an
almost interminable series of Notes by M. Tombeck have led to the
development of a classification which is exceedingly complicated, and
which in several important points it seems impossible to accept.
As published by MM. De Loriol, Royer, and Tombeck (50), and
modified by the last named (5d), it is as follows :—
PoRTLANDIAN.
1. Zoue of Cyrena rugosa.
a. Upper grey-green limestones.
6. Vacuolar oolite.
c. Lower grey-green limestones.
. Zone of Cyprina Brongniarti.
a. Tubulous limestones.
6. Spotted limestones.
¢. Carious limestones.
3. Zone of Ammonites gigas.
a. Bure oolite.
6. Limestone with Amm. irius.
¢. Marls with Hemicidaris purbeckensis.
d. Lithographic limestone with Amm. rotundus.
bo
KIMMERIDGIAN,
1. Zone of Amm. caletanus, = Virgulian.
a, Alternations with Amm. erinus.
6. Marls with Amm. eumelus.
2. Zone of Amm. orthocera, = Pterocerian.
a. Perforated limestones.
b. Marly limestones with Dysaster granulosus.
¢. Limestone with Jsocardia striata.
d. Marls with Rhabdocidaris Orbignyana.
e. Marls with Ceromya excentrica.
Jf. Perforated limestone with Pteroceras.
CoRALLIAN OB SEQUANIAN.
1. Second zone of Zerebratula humeralis.
Astartian limestone. -
2. Second zone of Cardium corallinum.
La-Mothe oolite.
3. First zone of Zerebratula humeralis.
a. Lithographic limestones.
6. Saucourt oolite.
ce. Limestones with Nautilus giganteus.
d. Upper rubbly limestone with Cidaris florigemma.
é. Limestone with Amm. achilles.
f. Limestone with Amm. bimammatus.
4. First zone of Cardium corallinum, and zone of Hemicidaris
crenularis.
a. Upper maris without fossils.
b. Diceras-oolites, and lower rubbly limestenes with Cidaris
florigemma.
¢. Lower marls without fossils.
OXFORDIAN.
Zone of Amm. transversarius.
a. Beds with Amm. Henrici and Amm. oculatus.
6. Beds with Amm. Babeanus.
¢. Beds with Amm. Martellé.
518 J. F. BLAKE ON THE UPPER
This is an exceedingly complicated classification ; but it 1s neces-
sary to give it in full, because points of discussion arise depending
on its details. According to the descriptions given by Tombeck, all
kinds of extraordinary developments of the Corallian rocks take
place in this district, and many differences are observable from any
Fig. 5.—Map of Part of the
Valley of the Rognon.
(Scale 1 : 80,000.)
thing found elsewhere; but though
it may seem presumptuous to found
any opinion upon a rapid survey, yet
that survey, directed to the special
examination of crucial spots, fails to
reveal any thing very abnormal,
though there are considerable differ-
ences when the rocks are compared
- with those already studied. In point
of fact, an examination of the locality
fails to comfirm M. Tombeck’s con-
clusions in several important points.
The chief point necessary to esta-
blish is the true succession of the
rocks which lie between the Virgu-
lan and the Oxfordian beds. By
the aid of a personal examination of
the spots, aided by the definite facts
recorded, when rightly interpreted,
one may come to a pretty sound con-
clusion.
« This portion of the series may be
- first examined in the valley of the
Rognon. Passing down this valley
from Andelot towards Donjeux, the
Corallian rocks, in the form of rubbly
limestones with Cidaris florigemma,
are first seen on the left bank of the
stream at Roche-sur-Rognon. Their
base is not here well exposed; but
is stated (19) to consist, in the neigh-
bourhood, of disaggregated oolites
with Glypticus hieroglyphicus, over-
jain by. white coral-limestone. On
the opposite. side of the stream the
rubbly - limestones are themselves
absent, their place being taken at
Cultra by compact Oxfordian lime-
stones, similar to those which occupy
so much of the ground below them
(by general dip) on the left bank.
This is doubtless due to a fault;
though Tombeck (65) actually thinks
the rubbly limestones 100 feet thick
have changed into this compact well-
JURASSIC OF THE PARIS BASIN. 519
stratified form at a distance of 500 yards. A second cross fault
cuts off Cultra from the cliff of Bettaincourt, where the great
Diceras-beds occupy the ground down to the stream. ‘The relation,
therefore, of the two parts of the Corallian rocks is not here so clear
as could be wished; but some portion of the Diceras-beds are seen
to be lying on the top of the rubbly limestones further back at
Roche-sur-Rognon; and at Reynel, about 3 miles to the east, Tom-
beck (55) describes an admirable section, having at the base Ox-
fordian marls with O. dilatata, then grey marls with Cidaris flori-
gemma and Hemicidaris crenularis, next a mass of coral limestone
with corals in situ, gradually becoming oolitic and then pisolitic as at
Bettaincourt, the whole being 300 feet in thickness. Notwithstand-
ing this section, however, he thinks (65) that the one form changes
into the other.
The Diceras-beds at Bettaincourt, first seen here in a journey
westwards in their full development, are marvellous deposits. They
consist of rolled fragments of all sizes, coated with calcareous cement,
and which in one sense may therefore be called oolitic grains; but they
have been subjected to a very different variety of the process which
produced the concentric coats of the latter. In oolites the process
is tranquil, in these tumultuous and rapid, the whole presenting the
appearance of a substratified heap of rubbish from a neighbouring
centre of life, borne along by the ancient currents which swept
through the straits of Dijon. Such beds might be supposed to re-
place, with almost any rapidity, the coral-growths from which they
are derived, or to die out entirely. There are, however, great
varieties in the Diceras-beds themselves—pisolites, large-grained
oolites, suboolitic, and thin-splitting limestone alternating; and
various groups of fossils are found in the various parts; but yet
the whole is indivisible. With many Dicerata occur Cidaris flori-
gemma, Cardium corallimum, and many rolled sponges. The other
fossils noted were Nerinea sequana and other species, Littorina
muricata, Isocardia striata, Corbis gigantea, Lima leviuscula, L.
pectimformis, Trichites sp., Ostrea pulligera, and Terebratula mal-
tonensis. What the real thickness of these beds may be it is im-
possible to say; their stratification is so irregular, and their change
of character in a lateral direction so marked, that all estimates are
worthless. Perhaps 300 feet may be seen in the Bettaincourt hill-side if
there is no real dip ; but even more may be introduced in the five miles
over which the deposit spreads. It is, of course, easy (50) to pick
out one of the oolitic portions, and call it the “ oolithe de Saucourt,”
and another above this, and call it the “ oolithe de La Mothe;” but
the actual oolites which occur at those places are not thereby proved
to be superimposed, unless they are proved identical with these
beds, which has not been, and cannot be done. The whole forms
one great mass (here at its maximum of development), representing
on the one hand the Novion and Vadonville limestones, and on the
other the whole mass of the Diceras-beds further to the west. The
upper portion is certainly more compact than the lower. On reach-
ing Saucourt the peculiar character of the Diceras-beds is lost; and
520 J. F. BLAKE ON THE UPPER
on ascending the hill we find the oolites above worked in a 12-foot
face, and overlain by a shelly limestone crowded with Rhynchonella
pinguis; this is followed by more compact limestone, some portion
of which may possibly be slightly oolitic; but there is nothing re-
markable to distinguish the whole series, nor is its relation to the
Diceras-beds below very clear.
Succeeding these compact limestones comes no great thickness of
irregular limestones, such as have been seen to characterize the
Astartian beds near Gondrecourt ; and on the top of the hill follow
the marly beds with Hxogyra virgula im lumachelles, and Phola-
domya acuticosta. If any Pterocerian is to be made out here, it
must be by a very close examination of fossils, which are not by any
means abundant.
At the forges of Donjeux, about a mile further on, is a quarry in
which the oolite of La Mothe is supposed to be seen. Here the top
beds consist of the irregular Astartian limestones; and the base of
the quarry is worked for massive rocks, which are on the whole
compact, varying on the one hand to lithographic stones, or on the
other developing a fair proportion of oolitic grains, but totally un-
like the Diceras-beds, because like any other semioolitie rock. Here,
then, is no repetition; and on the whole, with the exception of
the remarkable Diceras-beds, the succession in this valley is very
similar to, and certainly consonant with, what we saw in the last
section in the Meuse department. The chief noticeable point is that
the peculiar pisolitic character is exhibited rather at the base than
towards the top of the mass.
Fig. 6.—Map of Part of the Marne Valley. (Scale 1: 80,000.)
NY ty : cs
y Buxr xere8//1/ of fH e' 4 a
i j (Conf. z) Us, Bl eens) >
1a bal Be e
ee
psiheem fet pb. L,
ISG (erga) eds)
Favin a
2 Joe ers
o fre TAN ay a fptee care) €or. ool}
Bam HS Opforaisn) _|
Now let us pass to the valley of the Marne. A complete section
of the lower portion may be obtained by following the right bank
of the river from Vouécourt to Buxicres, and then mounting the
JURASSIC OF THE PARIS BASIN. 521
hill-road. The base of the hill called “ Les Lavicres ” is formed by
well-exposed sandy marls and flaggy beds, which are very poorly
fossiliferous, and appear to represent the ‘‘ marls without fossils,”
the only fossils obtained being Amm. marantianus and Area rhom-
boidalis, the latter a fossil of wide range. The amount of this
material must be considerable; in fact, in the neighbouring cutting
of Buxieres about 50 feet is seen. Above these marls, on the road
running north, are quarries of rock somewhat slipped out of place,
but consisting of solid blocks of true oolites with Amm. plicatilis—
a very good representative of a “coralline oolite.” Soon a river-
cliff is reached, by the side of which the road runs, and we have
a continuous section with scarcely a break. First there is a shell-
limestone, in parts oolitic, containing Chemnitzia heddingtonensis,
Neritopsis Guerrei, Cerithium mornatum, Nerinea sp., Trigona Etal-
lon ?, Lama leviuscula, Pecten articulatus, Ostrea solitaria, Rhyncho-
nella corallina?, R. pinguis, and Terebratula rotundata?. There are
also numerous corals; in fact, in places towards the upper part the
rock becomes a complete reef; but the corals are not commonly
Thamnastrean, and the urchin is C. Smthit and not C. florigemma.
Nevertheless these coral-growths must represent the Rag ; for, traced
upwards, the rocks become more oolitic, then pisolitic, and finally,
without our being able to draw any line, we are fairly launched into
the characteristic Diceras-beds with all their great masses of rubble,
their Diceras and Cardium corallimum. The whole of these beds
constitute a magnificent assemblage of limestones which can scarcely
be less than 300 feet in thickness. There is no change here in a
horizontal direction, as stated by Tombeck. The beds dip slightly to
the north, which brings higher beds to the same level; but the
Diceras-beds are not met with till we begin to mount; it is there-
fore, on the contrary, a vertical succession. The beds which overlie
the Diceras-beds here gradually lose their pisolitic character and
become marly and rubbly, but are often compacted into solid blocks.
The fossils observed in these beds were Pholadomya Protec, Ceromya
striata, Mytilus perplicatus, Trichites sp., Ostrea gregaria, and Tere-
bratula Leymerw. These beds represent, apparently, the subdivisions
C to F of Tombeck’s first zone of Ter. humeralis, and have a thickness
of about 60 feet. They are here followed by a somewhat more oolitic
block capped with a bed of Rhynchonella pinguis, which may well
be the continuation of the block quarried at Saucourt. Above this
come compact, nearly lithographic limestones, which occupy all
the summits of the hills. The whole succession is here therefore
perfectly clear, and it is singularly ike what has been recorded as
seen at Reynel.
There is nothing in all this to indicate any thing abnormal, fur-
ther than the characteristic inconstancy of the Corallian recks. The
Oxfordian strata, however, appear to have put on a different facies.
There is here no Calcareous Grit with characteristic fossils, nor any
Ferruginous Oolite ; and the species of Ammonites are not those which
are common to the east. Further down in the Oxford clay the zones
appear to be continuous, and hence the new form of marls with
o22 J. F. BLAKE ON THE UPPER
Ammonites marantianus &c. must have taken the place of the upper-
most portion.
On account, however, of the many questions which have been
raised about the Haute Marne, taken by the French geologists as
their typical area of Corallian rocks, it is needful not only to make
out the succession from the rocks themselves, but also to discuss the
evidence brought forward in support of a different and more complex
reading. The peculiar changes supposed to be here effected in the
relations of the recognized Corallian rocks and those hitherto con-
sidered Oxfordian, and the generalizations founded on this, have been
developed by degrees in numerous papers by M. Tombeck (45, 48, 50,
55, 57, 58, 64, 65, 66).
The ‘“ Marls without fossils,” stated by M. Royer to underlie the
Corallian, were first made to be their lateral equivalents (55), and
afterwards (64) were divided into two parts ; and the whole Corallian
mass, when that occurred, was inserted between the two, which unite
into one in its absence. Hence the fossils of these barren marls, espe-
cially Amm. marantianus, were considered Corallian; and wherever
that species is found we are to look for the Coral-beds and Pisolites
beneath it. Hence, too, the beds with Amm. tenwlobatus, which are
said to come above those with Amm. marantianus, are to be placed in
the Astartian instead of the Oxfordian. Now, whatever evidence
there may be elsewhere to show the true position of these zones, the
only evidence obtainable from the Haute Marne shows that the first
zone lies below the Corallian.
The idea that the Corallian rocks change into marls depends on a
comparison of the series in the valley of the Marne with that in the
neighbouring valley of the Aube, and will be discussed later. The
newer idea that they are to be intercalated is supposed to be proved
in the valley of the Marne itself.
The river-cliff before mentioned, which skirts the right bank of
the Marne from Les Laviéres to Buxiéres, forms a semicircle of rocks
haying a fairly constant dip to the north. The radius of this semi-
circle is 1500 yards; and near the centre is a low hill, through which
the railway passes in a cutting at a distance of only 1000 yards
from the cliff. In this cutting it is said that the Diceras-beds, 300
feet thick at 1000 yards distance, have died out to a thin wedge,
and may be seen lying in the midst of the marls(65) and the under-
lying rubbly limestones at the base. Neither of these statements
can be accepted. ‘The marls at the cutting are the continuation of
those of Les Laviéres, with exactly the same character: there are hard
bands in them; but these are not Corallian ; and the top of the cut-
ting on either side is covered by the shelly limestones of the cliff
and their fragments, with corals and Pecten articulatus &e. Here,
therefore, the Oxfordian marls are seen to underlie the Corallian
limestones. The Corallian limestones lie very slightly unconform-
ably on the marls; so there may be something wanting here.
Another locality supposed to prove the same is at Vouécourt,
two miles to the south (62). Above this village is a ravine leading
east (Ravin du Heu), and a road sloping up the hillside to Viéville
JURASSIC OF THE PARIS BASIN. ae
on the south (Cote du Noeulon). In the first the marly limestone
“4 A. Holbeim et A. marantianus” is said to be seen above the
Diceras-beds ; and in the second the Diceras-beds are said to be re-
duced tv almost zero in the midst of the clays. If “A. marantianus
is found” (in beds which lie?) “‘ above 50 metres of Diceras-beds at
Baxicres,” and (in beds which le?) “above 30 metres of the same
at Heu,” still one swallow does not make a summer, and the rare
occurrence of such a fossil would no more make the zone of Amm.
marantranus Corallian than the occurrence of species so near to Amm.
cordatus that they cannot be distinguished in Supracoralline or even
Kimmeridgian beds makes the zone of Amm. cordatus a part of the
Kimmeridge Clay. The actual section seen at Vouécourt is quite
consonant with all that has been seen before, except that in the
Ravin du Heu the lower part of the section is much distorted, and
the Corallian beds on the north appear to be let down, as by a fault,
to too low a level in relation to the Oxfordian on the south. The
section commences at the top with compact limestones, as at Buxieres;
then, below, come rubbly lhmestones with abundant Terebratula
Leymern, T. tetragona, &e., also Rhynchonella pinguis, Plewromya
Volizu, Anatina magnifica, Mytilus perplicatus, Pinna granulata, Pec-
ten inequicostatus, and Nerita Royert. Next follow marls and marly
flags containing the same Brachiopoda, Mytilus, and Pecten, with
Arca rhomboidalis and Pholadomya cor? ‘These are the beds which
contain Amm. marantianus, according to Tombeck ; if they do, it has
not its usual associates, and is therefore out of its place. Below
comes a great mass of limestone capped by a rosy large-grained
oolite ; but the base is not seen, the whole being so disordered. In
these were seen Lima leviuscula, Pecten articulatus, and Rhyncho-
nella corallina. No doubt the Diceras-beds do not here make such
a show; but the succession above shows that we are at their top,
and there may be much more than appears. It is below all this
that the whole road along the Noeulon is cut; and it shows only
the marls and marly limestones of the Les-Lavicres and Buxiéres
cuttings.
All the other sections in and near the Marne valley quoted by
Royer or Tombeck, and those seen by the Geological Society of
France on their visit in 1856 (19), are perfectly consonant with the
present reading, and may be easily interpreted.
To complete the account of these lower beds, as developed in the
department of the Haute Marne, we must make a digression towards
the west to Maranville and La Mothe. At the first locality on the left
bank of the Aube we are supposed to recognize the Corallian in the
midst of the marls; there is, however, nothing Corallian about them.
The rocks seen in the hills here are a series of marly limestones far
more argillaceous than any seen before, having a thickness of 120
feet. They are most lithographic above, and most marly below, the
intervening portion being most fossiliferous. The fossils seen are Ox-
fordian, viz. Alaria bispinosa, Astarte striatocostata, Littorina Meriani,
Ostrea multiformis, Exogyra spiralis. There is nothing, therefore,
here to identify any portion as having a position above the Diceras-
a24 J. F. BLAKE ON THE UPPER
beds ; but the whole corresponds to the marls below. Though nothing
is seen above these Oxfordian rocks on the left bank of the Aube,
the whole country on the right bank to near La Mothe is occupied
by limestone rocks very similar in character to those at Buxiéres,
though only occasionally observable. At La Mothe itself the most
characteristic rock is exactly of the Doulaincourt and Buxieres type,
and totally unlike any thing called La-Mothe Oolite elsewhere ;
beneath it is a thick mass of large-grained oolite (perhaps 30 feet),
worked for building-stone at Curmont, below which here, in an exca-
vation, are seen the shelly limestones as at Buxieres. The succession
is exactly the same, and the fossils similar.
In Royer’s first description (4) these Diceras-beds were placed on
the same level; and it was after his visit to the valley of the Yonne,
where two Oolites are developed, that he endeavoured to find two
also in the Haute Marne. The Oolite at La Mothe lies on a mass of
compact limestone, which he traced to Soncourt, and there found
rubbly beds at the base. These rubbly beds he apparently took
for the thinned representative of the whole of the Corallian.
Numerous sections seen and described show that (as at Buxieres)
the base of the Corallian is rubbly and Coralliferous ; but it has
never been proved that the Oolite of La Mothe overlies any such
beds as the rubbly and oolitic limestones which cap the Diceras-
beds at Buxieres; on the contrary, such beds, with their usual
Brachiopoda, are seen above the Oolite in the neighbourhood of La
Mothe ; and these are followed by compact, almost hthographic lime-
stones; but whether immediately or not cannot be certainly made
out. Above these come the irregular limestones which usually in-
dicate the Astartian zone; and on the hill of Colombey-les-deux-
Eglises are the marls full of Ewogyra virgula, the whole being very
parallel to what is seen above Saucourt. The difference in elevation
between Curmont and Colombey is about 150 feet.
On the undisputed Astartian and Virgulian of the Haute Marne
no special observations have been made; but it may be noted that
the Geological Society of France found in the rubbly limestones of Don-
jeux, associated with several Merinwe, Natica hemispherica, N. turbr-
niformis, Pholadomya Prote, Plectomya rugosa, Ceromya eaxcentrica,
C.obovata, Hxogyra virgula, Ostrea solitaria, Rhynchonella pingus(?),
Terebratula subsella, T. Leymeri, and Holectypus corallinus. From
Joinville northwards we have the most complete development within
the basin of the “ Portland” rocks. At that town great masses of
lithographic limestones are quarried, all with the peculiar clay bands
dividing them into thin blocks, and containing virgulian lumachelles
here and there. They have a great thickness, and are very unfos-
siliferous; there are some alternations of marls and earthy lime-
stones. and a block of oolite at what may be conveniently called the
top. The Ammonites that have been found in them—A. gigas, A.
suprajurensis, and A. rotundus, together with Trigoma Pellati, T.
Cottaldr, Cardium Foucardi, Myacites jurassi, Pecten suprajurensis,
with others recorded by Tombeck, are sufficient to correlate these
limestones with what has been known elsewhere as Lower Portlan-
JURASSIC OF THE PARIS BASIN. 525
dian, though the facies is too different to permit us to compare it
directly with the portion of the English Kimmeridge Clay corre-
sponding to it. The next portion of the series, called by Tombeck
the zone of Cyprina Brongniarti, consists of three subdivisions, each
of which has sufficiently marked lithological characters to be recog-
nized without fossils; and they are admirably shown to the north of
Joinville. The thickness of this portion is estimated at 160 feet, and
it is far more fossiliferous than the lower group, as we have seen it
to be near Bar-le-Duc. Still the line between the two may be con-
sidered arbitrary, and very probably does not correspond to the
subdivisions in the Department of the Yonne. Pinna suprajurensis,
after which the series is named in that locality, occurs here in
abundance in some beds above the Bure Oolite, which are not cari-
ous. The whole is well seen above Rachécourt, as Tombeck says.
The chief fossils observed in this series are Cyprina Brongnarti,
Mytilus waunensis, Anatina incequilatera, Corbula mosensis, Cardium
Dufrenoycum, Cyprina implicata, Pecten nudus. These beds are
here better developed than in the Meuse, and yield more data for
comparison. ‘They are succeeded by a small thickness of unfossili-
ferous, dirty-coloured stones, which form the possible representative
of the “‘ Middle Portland” of Boulogne.
Above all these rocks, and seen in several places to continue
without discordance into them, are the remarkable beds placed as
the “ Zone of Cyrena rugosa.” They partly consist of grey flags,
sparkling with minute crystals and crowded with Corbula? inflewa,
and partly of vacuolar oolite, worked in thick beds free from fossils,
having here and there bands of shells, the principal of which are
Astarte rugosa, Corbula inflewa, and <Avicula rhomboidalis. The
beds have the appearance of having been formed in shallow water.
These rocks, of which the 16 feet worked at Chevillon may be a
maximum, appear to be separated from all below them, both in
character and the greater number of the fossils; and under these
circumstances, perhaps, the single shell (Astarte rugosa) which they
have in common may suffice for a bond of union with the English
Portland rocks. The development here is extremely restricted, these
rocks not having a range of more than 30 miles.
4. Department of the Aube.—We here come under the guidance ot
Leymerie (7), whose work, though now old, is admirable; and very
little attention appears to have been paid to the department since
his time. His classification of the rocks is as follows :—
Upper JURASSIC.
1. Portland limestone, 330 feet.
2. Marls and limestones, with Hxogyra virgula, 250 feet.
MIDDLE JURASSIC.
1. Astartian limestone, 320 feet.
2. Nodular white limestones= Coral Rag, 40 feet.
3. Lower Coral limestone.
a. Compact limestone, 80-100 feet.
b. “ Levique” limestone, 50 feet.
e. Oolitic shell-limestone, 80-100 feet.
Fig. 7.—Map of the Valley of the Aube, near Bar.
526 J. F. BLAKE ON THE UPPER
Our first traverse is down the valley
of the Aube, on either side of Bar-sur-
Aube. At Clairvaux, not very far north
of Maranville, near the river, there
BY fae” are great cement-works, where cement-
We Sai const
tema stones, more or less sandy, and inter-
\\ eles spersed with marly beds, are worked over
os a thickness of 40 feet or more. These
contain abundant fossils ; the chief noted
were Cerathium muricatum, Pholadomya
canaliculata, P. cngulata, Trigona per-
lata, Anatina magnifica, Goniomya sul-
cata, Pinna lanceolata, Gervillia avicu-
loides, and Exogyra spiralis. There really
cannot be very much doubt whereabouts
we are in the series here; it must be
the top of the Oxfordian, somewhere on
the level of the Lower Calcareous Grit.
These, in fact, appear to be the beds that
are missing a little further to the east
(at Buxieres), and probably on a higher
horizon than those at Maranville. In
any case the fauna is perfectly distinct
from that of the somewhat marly lme-
stones which le above the Diceras-beds
at Vouécourt. In Leymerie’s lists no
such assemblage is noticed ; and it would
seem that these beds were not open to
his observation.
The immediately overlying rocks are
not well observable here; but there ap-
pears no sign of rubbly Coral Rag or of
Diceras-beds, in place of which the
marly beds become more sandy, then
more solid, and finally change into a
massive limestone. ‘This is not to he
wondered at, when we observe the great
reduction the Diceras-beds have suffered
between Buxicres and La Mothe. We
are here introduced, in fact, to the fea-
ture which characterizes much of the
western extension of the Upper Jurassic
rocks: they tend more and more to be-
come a uniform mass in which recog-
nizable rocks of peculiar constitution
are mere occasional occurrences. The
solidity of the limestones in this dis-
trict is well shown in a quarry-face
of 60 feet, the base of which is reached
by a continual ascent through a stony
JURASSIC OF THE PARIS BASIN. DOT
ravine; and here, high above the cement-stones, perhaps 200 feet,
we find a fossiliferous zone, similar to that at Saucourt, belonging
to the compact limestones above the Diceras-beds. This contains
Arca lineolata, Mytilus longevus?, Trigonia Etallom, Avicula obliqua,
Pecten suprajurensis?, and Rhynchonella pinguis. Towards the
top of the quarry the limestones become chalky. ‘These great masses
of course occupy the country for several miles; and thus we find this
same fossiliferous zone three miles to the north at Bayel. Here, too,
the Rhynchonella-bed lies at the base, and the upper part is chalky.
Cladophyllia occurs here and there; and in addition to the same
Trigonia and Avicula, there are Pecten vimineus?, Cyprina callosa,
Roém.?, Lerebratula tetragona, and Cidaris Smuthu. Traced still
further upwards, the rocks become lithographic and unfossiliferous.
The whole of this mass was considered Astartian by Leymerie; and
hence he gives 320 feet as its thickness; but it plainly represents
every thing which lies between the Oxfordian and Pterocerian.
The next recognizable beds are irregular somewhat marly lime-
stones, with Pteroceras Ponti and Mytilus acinaces. In such a mass
it is difficult to recognize Astartian beds ; but it seems probable that
some part at least of the lithographic limestones belong to them ;
and hence the overlying beds, which are irregular in character, and
contain one of the characteristic fossils, are the best representatives
of any thing that could be called Pterocerian that has been hitherto
seen. On the north of Bar-sur-Aube the marls with Hvoqyra
virgula are well exposed, but do not yield many fossils, the chief
noticed being Pleuromya tellina. This portion of the series pos-
sesses but little interest, but is followed by the * Portland” litho-
graphic limestones similar in character to those at Joinville, and
containing a plicatiloid Ammonite like A. beplex. Above this
is seen, near Bossancourt, another important Oolite in this series.
Tt is the one which, in the Haute-Marne, is called the Bure
Oolite® here developed to a bed of considerable importance, more
than 6 feet in thickness, and worked in underground mines for
building-stone. It is singularly free from fossils ; but below it are
some dirty-coloured oolites, with Amm. suprajurensis and small
oysters; whilst above are thin-bedded rather chalky limestones,
with oysters also, and the following fossils—Cardium Dufre-
noycum, Cardium Verioti, and Trigonia truncata. These pass into
varying limestones, amongst which are the beds containing great
branching earth-filled hollows, hence known as the carious lime-
stones. They are well developed—partly chalky, partly rubbly—
all the way to Trannes, where a large quarry shows the last of the
jurassic rocks in this district. In these beds, which would probably,
if searched, reveal a good fauna, occurred Lima suprajurensis, L. bo-
loniensis, Pecten suprajurensis, Lucina fragosa, Terebratula subsella
(var. minor), and teeth of Lepidotus. We here therefore do not see
beds so far up in the series as those of the Marne valley, no repre-
sentatives of the spotted limestones or of the vacuolar colite being
preserved ; but the lower portions seem to become more and more
fossiliferous as we pass westward.
528 J. F. BLAKE ON THE UPPER
Reel)
CON ec (acs)
i RA ia THAME
ANS al Mt
uh
eed)
SS
~ 1) =" os
ealtes LeVannage
Ruf \Ss
(Oxf Gril € , ae
Lani nee a ren Pee a a
The next traverse, though not along the valley of a river, is an
exceedingly instructive one, as we get an almost complete section
from the Corallian to the uppermost beds. ‘This is across the hill
that intervenes between Gyé-sur-Seine and the Riceys in the south-
western portion of the department. Commencing at the former
place, we find a cliff cut at the road-side, and all the rocks laid bare.
At the base is (1) shelly limestone, similar to that at the top of the
Clairvaux section, with indications of bastard oolite, like the Di-
ceras-beds of Doulaincourt, and containing crinoid stems and Rhyn-
chonella pingus. There is therefore still an absence here of the great
Diceras-masses ; and thetypeis conformable to that of the valley of
the Aube. Next (2) are from 30 to 40 feet of chalky limestones, split-
ting into rather thin layers, with Pholadomya congulata, P. cor ?, and
Amsccardia Legayt. Above this comes (3) a 2-foot band of a curious
blue earthy limestone, with globular masses of calc tuff. This seems
to be a bed of separation between two groups of rocks; it contains
few fossils, except Pholadomye (cf. P. ampla). If any definite
JURASSIC OF THE PARIS BASIN. 529
line therefore can be drawn, it is above this that the Astartian zone
should commence. Next comes (4) a mass of about 30 feet of solid
light-coloured sublithographic stone, with two bands of remarkable
character, made up of rolled fragments recemented, with Natice,
Pecten striatus, Ceromya wabrensis, and abundance of Terebratula
Leymerti. It is just such a band as this that Prof. Hébert (31)
elsewhere thought a good line of separation, showing the distinctness
of Astartian and Corallian beds; but, as it is obvious that they
cannot both be such, they both lose their importance, and prove that
there were frequent changes in the deposits about this period. This
same feature is indicated by subsequent deposits in this section, in
which are many rubble-beds alternating with lithographic lime-
stones and occasional oolites. Such beds have athickness of about
60 feet, and contain Pholadomya Protei, P. rostralis, Thracia tenera,
Pecten Tombecki, Terebratula Leymeru, Rhynchonella ? matro-
nensis, Cidaris Smithi, &ce. This is followed by the Virgulian
marls, full of Hwogyra virgula and Pholadomya rostralis, for
16 feet, exposed in the roadside, but extending far up the hill, and
finally surmounted by lithcgraphic limestone, with Terebratula
subsella. On continuing the route to the Riceys the descent of the
hill shows a second section corresponding closely with the first, until
the chalky limestones (2) are reached; but beneath these, instead
of the shelly limestones with only traces of Diceras, is a large deve-
lopment of true rubbly Diceras oolite, of which 15 feet in sheer
height are seen in one spot, although there may be much more of it.
These beds form the cappings of the hills, and assist in producing
the magnificent escarpments which overlook both sides of the river.
Wherever these Diceras-béds occur they never require to be looked
for; and where they do not form a marked feature it is pretty certain
they are absent. The principal fossils noted were Nerinea wmbili-
cata?, Diceras arvetina, Nerita Royerr?, Trigonia Ktallon, and Rhyn-
chonella matronensis. . Beneath these, on the west side of Ricey Bas,
is cc a mass of 6 feet of a compact oolite, with few fossils in a
crystalline state. Underlying this, again, is a considerable quantity
of white chalky limestone, tending to be flaggy on weathering, and
occasionally false-bedded. Of this there may be 60 or 70 feet, the
principal fossils being Pholadomya striatula, Avicula Gesneri, and
Rhynchonella pingms. In downward succession we reach, at Le
Vannage, a quantity of shelly limestone, with abundance of corals,
in which Pecten vimineus, Rhynchonella corallina, &e. abound, but
in which no Cidaris florigemma could be found. On crossing the
boundary into the department of the Cote d’Or, at a very slightly
lower level, there are numerous quarries in a calcareous grit, whose
horizon is accurately fixed by the occurrence of Trigonia spincfera.
In the last-named department there is a very considerable develop-
ment of the lower coral-beds, with Pecten vimineus and Rhynchonella
corallina, followed in regular succession by the Oxford grit and marls.
This traverse has been given in greater detail because it appears
to be a very important one, not hitherto noticed or described, and
serves for a term of comparison between the series of the Aube
Q.J.G.8. No. 148. QN
530 J. F. BLAKE ON THE UPPER
and Haute-Marne and that of the Yonne. The thicknesses given
by Leymerie must be maxima; but the succession he gives is well
made out. It is obvious that he reckons the whole down to the
Diceras-beds to belong to his Astartian: the first-named is his “* no-
dular white limestone,” though none of his lists of fossils contain
Diceras; and the underlying beds observed in the valley of the.
Laignes are his “lower coral limestone ” in its three subdivisions of
“ compact hmestone,” “ levique hmestone,” and * oolitic shell lime-
stone.” Now it has been seen that the Diceras-beds occupy the
position of the shelly limestone of Clairvaux and Bayel, and hence
we ought to find the true Coral Rag below in the Aube valley.
Unfortunately nowhere has Cidares florigemma been noted; but the
false-bedded character of the ‘‘levique” limestones, and the record
by Leymerie of a bed in them, at Gloire Dieu, entirely composed of
Crinoids (a feature so characteristic of the Coral Rag of the Meuse),
leads to the conviction that it is in these limestones we must look
for the representative of the Rag, and that the coral shell-beds of
the Cote d’Or must be regarded as “‘ Coralline Oolite,” so far as any
separation of these can be effected. On the other hand the great
development of beds below the Diceras-zone and the coralliferous
character of the base leads on to what we shall seein the department
of the Yonne, and show, to a certain extent, a repetition of the section
in the valley of the Marne.
5, Department of the Yonne.—The general description of the Upper
Jurassic rocks in this department is by Leymerie and Raulin, who
divide them as follows (25) :—
Upper JURASSIC.
1. Portland limestones, 135 feet.
2. Kimmeridgian marls and limestones, 330 feet.
Mipp.e JurASsIc.
. Astartian limestone, 83 feet.
. White coral limestone, 300 feet.
. Upper Oxfordian limestone.
. Middle Oxfordian limestones or marls, 260 feet.
. Lower Oxfordian ironstone, 33 feet.
Sue CO bD
Equally important, however, in this case are the subdivisions of
M. Cotteau (34, 42), though they are not very definitely formulated.
They are as follows :—
PoRTLANDIAN.
1. Zone of Pinna suprajurensis.
2. Zone of Ammonites gigas.
KCIMMERIDGIAN.
SEQUANIAN.
1. White limestones.
2. Lithographic limestones.
CoRALLIAN.
Diceras-beds.
OXFoRDIAN.
1. Zone of Ammonites plicatilis and Cidaris fiorigemma.
JURASSIC OF THE PARIS BASIN. 531
The lower portion of the Oxfordian is not brought into this scheme,
the last subdivision being in another scheme made the base of the
Corallian.
Two river-valleys cross this district, and the traverses made along
these give a complete idea of the development of the rocks under
consideration, which here attain their maximum in the lower part,
where they are truly marvellous.
Fig. 9.—Map of the Valley of the Armangon, south of Tonnerre.
(Scale 1 : 80,000.)
We commence with the valley ofthe Armancon. At Ancy-le-Franc
an admirable section commencing in true Oxfordian rocks is seen
above the church. Towards the base are marly beds, with only an
2n 2
Hae J. F. BLAKE ON THE UPPER
occasional calcareous band. ‘The fossils at once indicate the horizon,
those noted being Amm. tricristatus, A. Martelli, Pholadomya an-
gustata, and Arca rhomboidalis?. Traced upwards these marls
become more calcareous and are almost limestones. They are there
crowded with Pholadomya paucicosta, and have also P. flabellata, Cer-
comya antica, Pinna lanceolata, a Trigoma like T. perlata, and Pecten
demissus. ‘They become finally less fossiliferous, and are capped by
shelly limestones. This series may be traced with the same
character westwards to a great roadside quarry, where a face
of 40 feet of sandy limestone is worked, and so on to Pacy,
where the weli-xnown quarries have yielded many fossils, the
chief of which are Amm. ef. plicatils, Belemnites ? Royert, Pholado-
mya paucicosta, Myoconcha Rathervana, Trigoma ef. wrreqularis,
Pecten demissus, Exogyra spiralis, and, according to Cotteau, Ostrea
dilatata. There can be no doubt that these rocks represent true
Oxfordian strata; but their relation to those in the valley of Jully
has not been made out, though it is highly improbable that the
latter are older, as they contain, according to Leymerie and Raulin,
the characteristic fossils Ammonites perarmatus, Rhynchonella va-
rians, and Pecten fibrosus, which have not been found here. The
numerous changes thus observed in the character of the rocks which
underlie the Corallian must be due either to an unconformity or
to a very variable development of the Oxfordian strata; but we can
hardly accept the arrangement of the strata by the above-named
authors, who place the beds with Rhynchonella varians as the Lower
Oxfordian, while those at Ancy and Pacy are considered to be one
facies of the Middle Oxfordian, of which the other facies is the Coral
Rag, to be noted presently at Merry-sur-Yonne andelsewhere. ‘The
next succeeding series in this district is a mass of lithographic lime-
stones, tending to split into thin plates, and for the most part un-
fossiliferous. Here and there, however, in its mass are fossiliferous
zones, apparently the representatives of strongly characterized beds
further to the east. The lowest of these has not actually been met
with ; but it is very instructively described by Cotteau (43), as seen
in the neighbourhood of Gland, where the following upward suc-
cession is determined :—(q) ferruginous Oxford clay; (6) sponge-bed ;
(c) limestones of Pacy; (d) rubbly limestone; (¢) coral-bed, with
Pecten subarticulatus and Cidaris florigemma ; (f) lithographic lime-
stones ; (g) coralline limestone of Tonnerre. It is impossible not to
see in the beds ¢ and d the continuation of those of Vannage and
the Cote d’Or, the succession being perfectly consonant to what
we might expect. There are, however, other bands in the litho-
graphic limestones nearer the summit, one of which is seen on the
roadside west of Commissey, associated with a rubble-bed ; another
oceurs close to the village of Angy (below the white limestone),
where it was seen by Hébert (31), and considered to be a junction-
bed between the Corallian and Oxfordian, though lying upon one
great mass of lithographic limestone and covered by another. The
commonest fossil of this series is Rhynchonella coralliima. ‘This por-
tion, though, being more lithographic, it is less clearly characterized,
JURASSIC OF THE PARIS BASIN. 533
will occupy the place of the compact and “levique” limestone of
Riceys, if we find above it the representative of the Diceras-beds.
Above the lithographic limestones comes an enormous mass of
white chalky limestone, seen on the right bank of the Armangon be-
tween Commissey and Tonnerre, and on the left bank at the well-
known quarries of Angy and Tonnerre. The limestone of Angy is
celebrated for its fossils, which occur in profusion and in admirable
preservation. A face of 50 feet is worked, the rock being more sandy
towards the base, and having masses of Septastrea, large Monthvaltic,
Trichites Saussurer, Diceras sp., Rhynchonella matronensis, Terebratula
maléonensis, and Cidaris, apparently not C. florigemma. As this is the
<< White coral limestone” of Leymerie and Raulin, we find it credited
with 300 feet of thickness. This it might well be judged to have from
the hills in which it occurs; but it 1s not again well seen till the
great quarries near Tonnerre are reached; and here it has a 60-feet
face, which contains a different and higher portion, remarkable for
the great masses of banded flints which lie more or less in lines.
These are Nos. 7 to 15 of Cotteau’s section (34) and contain many
unusual Echinoderms. We here also find the overlying rocks,
which are, first, a solid block of 10 feet with rolled nodules and a
few specimens of Diceras and Lhynchonella pinguis, and next some
nodular and coralliferous beds. The corals are rolled and not wm situ
(No. 56 of Cotteau). Next comes a coarse oolite, and then another
rubbly bed with massive corals, Rhynchonella pinguis, Terebratula
Leymeriz, and many other fossils, but no sign of Cidaris florigemma
(No. 24 of Cotteau). On the opposite side of the river no good
exposures of the white limestones occur at present; but Cotteau
describes an important quarry, called ‘‘ Voceuses,” which contains,
amongst other fossils, Cardium corallinum, Glypticus hieroglyphicus,
and Cidaris florigemma. The upper part, however, is seen about 2
kilometres south of Tonnerre, containing but few fossils, but in
parts composed of white rubble of exactly the usual character. It is
plain, therefore, that all this mass must be considered a develop-
ment of the Diceras-beds of Riceys, in which the peculiar character
is less regularly marked, and the fossils are therefore somewhat
different. On this side of the river other quarries show rubbly beds
above, then sublithographic stone, and then another rubble-bed
full of Terebratula Leymern, which Hébert (31) regards as the base
of the Astartian, though we have seen near Gyé that there may be
several such overlying each other. Above comes a coarse brown
oclite, which may, or may not, be the same as that seen on the west
of the river. In any case the sequence on this side matches very
well with the Gyé section, in which also rubbly beds with 7. Ley-
merit were overlain by oolite. The upward succession is of no
particular interest here; but the lithographic stones which overlie
the oolites gradually become more chalky, and finally yield Evoqyra
virgula and Pholadomya acuticosta, beyond which the beds have
not been traced, as they are better known near Auxerre.
The next traverse is up the valley of the Yonne, where it is best
to commence with the uppermost beds. It has been seen that
534 J. F. BLAKE ON THE UPPER
Fig. 10.—Map of the Yonne Valley south of Aumerre.
(Scale 1; 240,000.)
= Harty Lith L)
Vallen
Y
iy 4
ty (
j R Yonne p |
f
aulty 2 Vilts }
=~ 72 Chatvaw, oe
WZ
oo y
P
| a BA J © 2
:
=S5550
Cotteau divides the “ Portlandian” rocks into two groups, the
upper of which is the zone of Pinna suprajurensis. This is very
well seen in the neighbourhood of Auxerre, and, like all these upper
rocks, is more fossiliferous as we go west. After the splendid
monograph by Loriol and Cotteau, it is superfluous to quote the
fossils, the great majority of which come from the upper portion.
We need only compare the series with those seen before. In the
JURASSIC OF THE PARIS BASIN. 53D
valley of the Yonne there is no oolite to compare with the Bure
Oolite ; but the fossiliferous beds here correspond in character and
fossils to the limestones of Trannes, and therefore to the “ various
limestones.” It is also possible that, from the unevenness of the
Neocomian denudation, portions of the higher zone, or “ spotted lime-
stones,” may be represented, as at Villefargeau; but the series is
certainly incomplete in its upper part; and the question of any passage
here into the Neocomian, which De Loriol propounds (42), cannot
possibly be seriously raised. The lower portion of the ‘“‘ Portlandian ”
rocks is well seen on either side of the Yonne valley, where quarries
eccur with a 40-feet face of a soft chalky limestone with intervening
beds of marl, in which there is occasionally a lumachelle of Hvogyra
vurgula. Some of the marls contain abundance of Thracia depressa ;
and the other fossils noted were Amm. gigas, A. suprajwrensis, A.
Gravesianus, Plectomya rugosa, Cyprina Brongnartc (in another
quarry), and Pinna granulata. These beds correspond in position to
the lithographic limestones of Joinville. The beds in this locality
have a gentle rise to the south, and the sequence can be well taken
up again near Vincelles and Bailly. The tops of the hills,here are
occupied by the “ Portland” limestone, beneath which come earthy
fossiliferous limestones with large examples of Terebratula subsella
and Pholadomya multicosta, which graduate downwards into marls
full of Hxoqyra virgula. The Astartian beds are not well seen in
any section; but they consist partly of solid and partly of rubbly lime-
stones, with bands of Terebratula Leymerii, containing Plectomya
rugosa. Towards the base the beds become oolitic, then nodular,
then bedded; then comes a 16-feet mass of brownish oolite* with Rhyn-
chonella pinguis, then 2 feet of solid limestone. Below this comes
an 8-feet block of solid character, here and there containing the
peculiar pisolite of the Diceras-beds, which forms the cap to a mass
of white limestones, varying from oolitic to chalky, and containing
Ceromya excentrica, Homomya compressa?, Nerineea pseudospeciosa ?,
Corbis gigantea, Trigonia Htallon, T. variegata, Pecten Tombeckt, and,
perhaps, Cidaris florigemma. The series thus described is ob-
viously identical with that seen at Tonnerre, with the exception
that there are no beds of rolled corals over the Diceras-beds. The
white limestones extend some way to the south, where they are
succeeded by lithographic limestones. The basement has not been
seen, but is stated by Cotteau (42) to contain Rhynchonella coral-
lina, Terebratula humeralis, and Pholadomya paucicosta. At Mailly-
la-ville are seen some 20 or 30 feet of very flaggy beds, succeeded
by 12 feet of oolite, and then a development of the most extraor-
dinary kind, totally different from any thing seen before and of great -
interest. Along the banks of the Yonne are fine hoary cliffs,
composed at first ef a rock resembling a consolidated cale tuff,
without any stratification and weathering into peaks; the fossils
are not so numerous as might be expected, though Pecten artrculatus
* Above this bed, Hébert (21) draws the line between the Coral Rag and the
Kimmeridge Clay.
536 J. F. BLAKE ON THE UPPER
and Rhynchonella corallina were noted. On the same level these
change into Diceras-beds of characteristic material, with many ex-
amples of that genus ; and finally, at Merry-sur-Yonne, an immense
cliff, 200 feet in height, and carved into fantastic shapes, frowns over
the river, and is geologically an unstratified heterogeneous mass of
Coral Rag, Diceras-beds, and rubble all together. Huge masses of
Thamnastrea, delicate branches of Caryophyllia, and fan-like growths
of Thecosmilia here and there ornament the surface ; and in the inter-
spaces innumerable specimens of Diceras, Cardium corallinum, stout
spines of Cidaris florigemma, and Trichites a foot in length are crowded
together. It is the finest example of a Coral Rag visible either in
the basin of Paris or anywhere in England, and it is, undoubtedly,
impossible to confound it with the much higher beds described as
occurring at Bailly. Rocks of this description form the boundary
of the picturesque valley through which the railway runs past
Chatel Censoir to Coulanges. At the latter place there is an almost
equally fine cliff, composed of a white limestone as beautiful as that
of Angy, though apparently on a lower level, being really only
a modification of the Coral Rag of Merry. Here, too, the fossils are
in profusion and perfect preservation ; the finest examples of various
species of Diceras occur, associated with Werinea Cottaldina?, N.
subnodosa, Cardium corallinum, Hinnites, Terebratula wsignis,
Cidaris florigemma, corals growing in reefs, and sponges. ‘This
great corallian development proves conclusively that Dvceras,
Nerinea, and Cidaris florigemma are not always characteristic in
any sense of distinct horizons, and that the lowest portion of any
possible rocks which may be referred to the Coralian may be
characterized by the latter species. If the series has been rightly
traced in our journey westwards, these great coralliferous masses
must be the grander development of the coral-growths of the base
of the series in the Aube, only represented by thin bands at the
base of the lithographic limestones in the valley of the Armancon.
Much discussion has arisen on the correct position of these lower
coral-beds. At first they were confounded with the upper Diceras-
beds and supposed to be repeated by some fault (3, 6). Certain
marly limestones developed at Vermanton, with a proportion of
Oxfordian fossils, were, at that time, considered to belong to Ox-
fordian strata (9,14). These Vermanton lhmestones were after-
wards proved by Raulin to overlie the Coral Rag of Chatel Censoir
and Merry (15); and as they were still considered by him as Upper
Oxfordian, it followed that the Coral Rag below should be called
Middle Oxfordian, and as such it appears in the monograph by
Leymerie and Raulin quoted above (25). Cotteau, however, showed
by an exhaustive examination of the fossils (16), first, that the Coral
Rag was essentially “Corallian” in the usual sense, and, secondly, that
the Vermanton marly limestones, though from their similar lithology
they appear more closely allied to the Oxfordian than to the coral-
beds below, yet, on the whole, are really Corallian. It is noteworthy
that though these marly limestones are quoted in the earlier deserip-
tions as marls ‘a Anum. marantianus” (15), the only Ammonite given
JURASSIC OF THE PARIS BASIN. 537
in Cotteau’s exhaustive list is Amm. achilles; of the other fossils,
Trigonia clavellata, Ceromya excentrica, Unicardium globosum,
Phasianella striata, and Cidaris florigemma are the most noteworthy.
These beds are believed by MM. Royer and Tombeck to correspond
to the marly beds overlying the Diceras-beds of the Haute-Marne ;
but by their position they must be part of the lithographic
limestones which underlie those beds, though overlying the basal
Coral Rag.
The true position of these rocks is further certified by continuing
the examination downwards. On the north side of the Yonne, at
Coulanges, are seen, below the beds already described, 12 feet or
more of uniform compact limestones with Gryphea dilatata, and
then some sandy limestones, like those of Pacy, but more false-
bedded and irregular, with abundance of Yerebratula bisuffar-
cnata, also Trigonia spinifera, Nerinea allica, and many corals
here and there. These, which are doubtless the same as the
siliceous limestone of Druies, correspond very well with what we
might expect, though under a form slightly different. It is at some
distance below these that the fossiliferous zone of Amm. transver-
sarius occurs on the road to Clamecy.
6. Department of Niévre—The only description of the Upper
Jurassic rocks of this department is by Ebray (32), supplemented
by some notes inthe paper by MM. Douvillé and Jourdy (60). The
series is thus described by Ebray :—
KIMMERIDGIAN.
Astartian Limestone.
CoRALLIAN.
Upper Lithographic Limestone.
Oolite with small Diceras.
Chalky Limestone.
Lithographic Limestone.
Oolite of La Charité with Diceras arietinum.
Marly Limestone.and Lower Lithographic Limestone.
ARGOVIAN.
Sponge-marls with Amm. canaliculatus.
The only traverse made in this district 1s along the valley of the
Loire, from La Charité to the north of Pouilly. At the former
place large masses of very marly limestone, having a markedly Ox-
fordian aspect, are worked, in which fossils are very rare, but from
which Amm.bimammatus and Amm. canaliculatus have been recorded.
These continue some distance; but halfway to Meves are large
quarries showing a 40-feet face of white limestone, with much of the
rolled pisolitic material characteristic of Diceras-beds; and that genus
here abounds, associated with Nerinwa. Had one never seen the
limestone of Coulanges, one would, doubtless, take this for the
ordinary Diceras-bed, and its low position would be a difficulty ; but
538 J. F. BLAKE ON THE UPPER
Fie. 11.—Map of the Loire
between Sancerre and La
Charité. (Scale 1: 80,000.)
i iy) \sy CA ha
Fiat SPACE. i |
ery
OrES
oat
UOve
‘Raxs
i
TEAL SE LEED Se
by iuy
A ois
PEE py
SSS eae
Vs
SS
= $< iower Dreerss
= -Seds)
Pe
Re
i
oe
there is no difficulty now in re-
cognizing it as the tailing off of the
great Coral-Rag-like mass which
characterizes the valley of the
Yonne, more especially as it has
not been recognized on the left
bank of the Loire. The whole
space between these quarries and
those of Pouilly appears to be oc-
cupied by barren lithographic lime-
stones, the thickness of which it is
impossible to estimate. The quar-
ries of Pouilly are worked in a
finely oolitic stone, somewhat
false-bedded and containing few
fossils ; this must correspond to the
white limestone of Tonnerre and
Vineelles ; and we should expect to
find representatives of the Diceras-
beds above: of these no evidence
was found at Pouilly; but Rau-
lin (3) and Douvillé and Jourdy
(60), speaking of the same beds
seen on the opposite side of the
river at Sancerre, describe a re-
gular Diceras-bed as attaining its
maximum there, though dying
away to the west. On the hill
north of Pouilly are seen, first,
lithographic limestones, then some
rubbly limestones with TYerebra-
tula Leymerw, and at the summit
the marls with Hwogyra virgula,
and no more is apparent in this
direction, though higher beds
might well be developed. These
present no special point of in-
terest, beyond showing the con-
stancy of this portion of the series
in contradistinction to the varia-
bility of the beds below.
7. Department of the Cher.—
Works on this department have
- been published by Fabre in 1838,
and Boulanger and Bertera in
1850 (10); but the most recent
description is that by Douvyillé
and Jourdy, above quoted (60).
These latter authors classify the
series as follows :—
JURASSIC OF THE PARIS BASIN. 539
KIMMERIDGIAN.
Limestone of Barrois.
Virgulian marls.
Astartian limestone.
A. Marls and nodular limestones.
B. Nerinzan Oolite.
©. Kucoidal marls and limestones.
CoRALLIAN.
Upper lithographic limestones with Amm. achilles.
D. Limestone with Pinna.
HK. Compact limestones.
Chalky limestone of Bourges.
Lithographic lmestones.
Sponge limestones, with Amm. marantianus, A. bimammatus, and A. plicatilis.
The first traverse in this department 1s in theneighbourhood of Bour-
ges, where the succession has been already well studied and described.
From 3 to 6 kilometres north of the city the Virgulian marls appear,
overlain to the north by lithographic limestones, belonging doubt-
less to the so-called Vortland, and at the hill immediately outside of
Bourges the different Astartian beds are seen. The highest are
earthy limestones, partially lithographic and often extremely marly.
The characteristic fossils are large examples of Ceromya excentrica and
Pholadomya rostralis, Terebratula subsella and Plectomya rugosa;
WNatica Royeri also occurs. The next seen are a few feet of rubbly beds,
becoming very oolitic below, and more like the corresponding rock in
the Boulogne area than any yet seen. It is the Nerinzan Oolite of
the authors quoted, and contains Nerinea Desvoidyi?, Trichites
Saussurei, Terebratula subsella, abundance of 7’. Leymert, Rhyn-
chonella pinguis?, Pholadomya rostralis, and Trigoma Baylei, the
last-named forming an interesting connexion with the rocks at Havre.
The lower fucoidal marls have not been examined ; but from the list
of fossils quoted, among which may be noted Mytilus perplicatus,
Plectomya rugosa, Terebratula subsella, and Rhynchonella pinguis, it
is obvious they form part of this series. On the south of Bourges a
different group of rocks occur, the upper part being lithographic,
unnecessarily divided into two parts. The fossils are few, and
belong to Pinna obliquata (a broad species), Lucina cf. imbricata,
and Terebratula ? tetragona. These are of considerable thickness, and
are underlain by beautiful white limestone, which betrays its origin
when closely examined. It is then seen to be an exceedingly fine
rubble, haying here and there larger grains, and becoming almost
like the Diceras-beds, to which it corresponds, and into which it
is said to change at Sancerre. Terebratula cncta and Rhynchonella
coralina are extremely abundant. Lima leviuscula, L. rigida,
and Corbis gigantea were also observed. In the old quarries of the
Chateau, what are probably lower beds are seen through 20 feet and
more. Here are abundance of massive corals, with Crdaris flori-
gemma and many shells, but fewer Brachiopoda. ‘This, then, is the
true Coral Rag as usually seen, and corresponds to the white lime-
stones of ''onnerre and Augy. Below this the beds have not been
examined, as they are stated to consist of a uniform mass of litho-
540 J. F, BLAKE ON THE UPPER
Fig. 12.—Map of the Country round Bourges. (Scale 1: 160,000.)
graphic limestone over a breadth of 20 kilometres, and to show
no signs of the lower limestone of Coulanges and La Charite.
Boulanger and Bertera, indeed, mention a coral limestone below the
lithographic, to be seen near Venesme, which may represent it; but
they correlate 1t with beds with Amm. hecticus, in which case it must
be Oxfordian.
In the last traverse of this range the swallowing up ofall portions
of this series into uniform lithographic limestones, below, at least, the
Astartian beds, is carried to its maximum ; for though, near Chapelle,
the white limestone of the old Chateau quarries is still seen to be
developed, it is much diminished in thickness, and the whole of the
weary way from that locality to Chateauneuf-sur-Cher, along the
borders of the river, is occupied by a dreary monotony of thick-
JURASSIC OF THE PARIS BASIN. 541
bedded, unfossiliferous, lithographic limestones. One peculiar fea-
ture, however, is to be noted. About two miles south of St. Florent,
and again at Lapan, at a lower level in the series, the soil appears
of a peculiar rich red colour, and at the latter locality the cause has
been ascertained. Instead of the ordinary limestones there are some
beds, at least 3 feet or 4 feet thick, of a crystalline irregular mass,
which are suggestive of the strangely altered rock produced from
corals and coral-brash; and in this mass are cavities filled with
large, round, concentrically coated, limonite concretions. It is by
the decay of these that the fields are covered with the red soil; and
they may be regarded as the last vestiges of coral-growths, the lower
of which might well correspond to the Coral Rag of Merry. As we
approach Chateauneuf the limestone becomes white and more marly,
but still almost, if not quite, unfossiliferous ; and it is only to the
south of the town that the canaliculate Ammonites set in, associated
with abundant sponges and Amm. bimammatus and Amm. Martelli,
on which little need be said, since they are so obviously Oxfordian.
It may be noted, however, since the authors quoted place these beds
as the base of the Corallian, that the first Ammonite to appear
going down is Amm. canaliculatus; and this is far above the
sponge-bed.
The valley of the Indre has not been examined ; but Douvillé and
Jourdy assure us that here even the white limestones are wanting,
and the whole mass between the Astartian and Oxfordian consists
of nothing but barren lithographic limestones, spreading over an
expanse of 30 kilometres from Levroux to Chateauroux.
Il. Tae rwo CHARENTES.
This district scarcely forms part of the Paris basin, being rather
the northerly extension of the Pyrenean, and will doubtless serve
as a term of comparison between the two. Nevertheless, being so
close to the termination of the great range, it 1s more conveniently
studied on the present occasion. The main question, however,
of which the solution has been sought, is the age of the so-called
** Portland” and even ‘‘ Purbeck” beds—whether there are, in fact,
in this area any rocks corresponding to those that are known by
those names in England.
1. Department of the Charente.—The Jurassic rocks of the depart-
ment have been described by Coquand (24), who divides the upper
portion as follows :—
Upper J URASSIC.
Purbeckian.
Portlandian.
Carious limestone.
Limestones with Nucula inflexa.
Oolitic limestone.
Limestone with Cardium dissimile.
Sands.
Kimmeridgian.
Virgulian marls.
Pterocerian limestones.
Astartian limestones.
542 J. F. BLAKE ON THE UPPER
MiIppLeE JURASSIC.
Corallian.
Oolite with Neringe.
Coral limestone.
Solid limestone.
Oxfordian.
Callovian.
The whole series, as seen between Rochefoucault and Angouléme,
is extremely calcareous, and no physical line can be drawn between
the Oxfordian and Corallian; every portion is more compact than
usual, and presents no such marked features as are often seen. The
Oxfordian near Rochefoucault certainly contains coralliferous beds,
and these give place to a sandy oolite. From Coquand’s descrip-
tion it appears that the uppermost portion of the Oxfordian contains
in some places such fossils as Pecten demissus, P. subfibrosus, and Rhyn-
chonella Thurmanni, and in others Amm. oculatus, A. crenatus, and
A. Henrici, and is followed by a brecciiform limestone, indicating that
the Corallian here also lies on different portions and is really uncon-
formable. The massive limestones of the last-named group occupy
a wide expanse of country, but finally give way to rather rubbly
limestones, doubtless the ‘‘Coral Limestone” of Coquand, which,
however, scarcely forms a “ Rag”; and these, again, are replaced
by compact suboolitic limestones, containing Diceras at Touvres, and
in which Coquand records several Nerinee and Cardium corallinun,
Terebratula insignis, and Rhynchonella corallina. It is obvious, there-
fore, that the succession, though somewhat obscure from the similarity
of the rocks to each other, is the same that we have seen in the great
range before the lower Coral Rag appeared. The Astartian beds are
not here of any great importance, consisting of marly limestones, with
Pholadomya rostralis and Ceromya excentrica. The fossils quoted
by Coquand, except the Astarte supracorallina (“minima”), are not
specially characteristic; and it is to be noted that he considers
some beds at La Rochelle, which d’Orbigny placed in the Corallian,
to be the calcareous representatives of these more marly rocks.
Traced upwards, however, they become still more marly, and
contain abundance of Evogyra virgula. Indeed this part of the
series is rather exceptional; and after seeing so much limestone
one’s eye is refreshed by the sight of veritable clay, extending
through a considerable thickness. These irregular beds may be
taken up again in the railway-cuttings north of Angouléme; but
the lower portion, distinguished as Pterocerian, which is to be seen
some six miles to the north, at Vars, has not been examined. It
appears from Coquand’s description to be more than usually distinct
in this district by its fossils, which include Nautilus giganteus,
Pteroceras oceant, Chemnitzia Danae, Pholadomya Prote., Mytilus
medus, and Ostrea solitaria. The Virgulian marls near Angouléme
are fairly fossiliferous, the species noted as associated with Hxogyra
virgula being Natica ornata?, Plectomya rugosa, Arca ef. rhombor-
dalis, Trigonia concentrica, T. monilifera?, Gervilliia kimmeridiensis,
JURASSIC OF THE PARIS BASIN. 543
Thracia depressa (towards the top), Mytilus virgulinus, Ceromya
concentrica, and Pecten suprajurensis; and to these Coquand adds
Ammonites longispinus, Pholadomya acuticosta, and Pleuromya
tellina. The rocks therefore which here underlie the “ Portland”
are the same that have been hitherto recognized as Virgulian, and
represent the lower, or at most the middle, portion of our English
Kimmeridge Clay. We are therefore prepared to find that here also
the “ Portland” beds are no higher than those usually so called. Now,
tracing upwards the beds towards Angouléme, we find aset of rather
rubbly fossiliferous limestones, containing Pholadomya decemcos-
tata, Trigonia concentrica, T’. ef. Bronnit, Arca laura, and Cerithium
septemplicatum. These rocks become more sandy by degrees, and
ai last form a peculiarly crisp calcareous sandstone. ‘The fossils in
this sandstone, as noted, are Pseudomelania gigantea, Corbis Rather-
wana, and Avicula Credneriana, all characteristic species of the
* Lower Portland.” No more is seen in this section, as the Hip-
purite limestone lies uncontormably upon the last-named stratum. ©
The higher beds of the district were therefore examined in the
neighbourhood of Jarnac. The section at Souillac could not be
verified as showing four subdivisions overlain by gypseous beds; but
much oolitic stone is worked to the west of Jarnac, as far as Chassors
and Nercillac, to a thickness of at least 12 feet; in this Cyprina
Brongniarts is the characteristic fossil. From the fact of this species
not being quoted, but in its place Cardium dissimile (only a single
doubtful example of which could be found), and from the similarity
of the casts of these two shells, is it possible to conclude that for
the latter we ought to read the former in Coquand’s lists? Still
something very like the Cardium dissimile was seen at Nercillac, and
also, as will be seen, in the Lle d’Oleron. The other fossils noted
at Chassors &¢. are those often accompanying Cyprina Brengniarta,
or belonging to a higher zone, viz. Cyprina implicata, Astarie
rugosa, Pecten nudus (= yarnacensis), Cardium Dufrenoycum,
Astarte regularis, Corbula mosensis, and Mactra insularum. Over-
lying these near Jarnac are more flagey beds, with many small
oysters at the base. Comparing this with the more complete
development in the Haute-Marne, the beds here shown belong
obviously to the zone of Cyprina Brongniarti; and as several of
the fossils indicate at least the upper part of it, though the
gypseous beds above give no clue to their age, and we are
therefore left without proof in this district of the equivalents
of the vacuolar oolite representing the true Portland, it 1s pro-
bable that such beds, though under a somewhat freshwater con-
dition, are actually reached, being represented by the so-called
« Purbecks.”
2. Department of the Lower Charente.—The rocks in this de-
partment, originally studied by d’Orbigny (14), have since been
more fully described by Manes (17), who divides them as
follows :—
544 J. F. BLAKE ON THE UPPER
Portlandian, 280 ft.
Gypseous beds.
Lumachelle limestones.
Tabular compact limestones.
Alternations of compact limestones.
Kimmeridgian, 260 ft.
White chalky limestone.
Marls with Lxogyra virgula.
Corallian, 330 ft.
Coral limestones.
Limestone with Nerineee.
Oxfordian, 550 ft.
Shaly marls.
Clays and marly limestones.
Whether the rocks in the Lower Charente are really different
from those in the Upper, or whether their exposure in the sea-cliffs
. gives a better opportunity for judging differences, certain it is that
in the neighbourhood of La Rochelle one is immediately aware that
one is studying the development in a new basin, and things are
changed. If, in fact, we examine the lists of d’Orbigny as given
in his ‘ Prodrome,’ we find that out of 222 Corallian species from this
locality, no fewer than 90, or more than 40 per cent., are peculiar,
while only 80 occur in any of the localities yet studied.
The Oxfordian strata are of particular interest as occurring at
Marans, whence the name of Ammonites marantianus is derived,
which indicates that we should expect the overlying ‘“‘Limestones with
Nerinee” to belong to the true Corallian series. The lower portions of
these occur on the north side of La Rochelle; but the upper portion
is the more fossiliferous, and occupies the first two headlands to the
south, viz. the Point des Minimes and the Point de Roux. Here they
are yery marly, with beds of limestone crowded with cavities formed
Fig. 13.—Map of the Coast round the Pertuis d’ Antioch.
(Scale 1: 240,000.)
SEA
DR aitipecul
SSS AyD:
2 SSN Se a7 adie
s f de Chatelailbo We S g
JURASSIC OF THE PARIS BASIN. 545
by fossils which have decayed, leaving their exteriors perfectly
moulded. The most abundant fossils are some large curved Montli-
valtie (M. subnigra, VOrb.?), various peculiar Nerinee, small Cerithia,
Mytilus pectinatus, Trigonia aculeata, VOrb., T. Tombecki? (LT. Me-
riant of dOrbigny, but not that species), and <Astarte bicostata.
Thus the common fossils are the peculiar ones, and one must fall
back upon more detailed lists of rarer fossils. Amongst those
quoted by d’Orbigny, the most important for correlation are Belem-
nites Royert (probably from the lower portion), Ammonites achilles,
Natica grandis, N. hemispherica, Turbo princeps, Cardiwm corallinum,
Mytilus acinaces, Lima leviuscula, Avicula polyodon, Pecten subartr-
culatus, Terebratula insignis, and Hemicidaris crenularis. None of
the others having a contrary tendency, it is plain that in the great
mass composing this series we have represented the shell-limestone
usually included in the Corallian, up to and including the Coral Rag
itself; though Crdaris florigemma does not appear to flourish here,
and the corals are not Astrzean. Passing south towards higher beds,
we find some more marly limestones with Pholadomya Proter and
— Pinna obliquata not uncommon. If the latter shell may be trusted
to keep to a single horizon, it should represent the lithographic
limestones overlying the chalky limestones of Bourges. However,
at the next point, Point du Ché, a fine development of a Coral Rag
is seen. This is credited with more than 200 feet by Manes; but
as the next series named is the Virgulian marls, it is obvious that
the Astartian beds are included in this. ‘The cliffs have a height
of 30 feet to 40 feet; and all is apparently Coral Rag, though on a
higher horizon than usual. Fossils like Arca tetragona, Lima verdu-
nensis, Terebratula, are abundant, with spines of Cidaris; to which
may be added from d’Orbigny’s list Nautilus qiganteus, Nerinea
Mandelslohi, Pinnigena Saussure, Diceras arietinum, and Rhyncho-
nella pinguis (“ mconstans’’).
This portion of the series may therefore fairly be placed on the
horizon of the Diceras- or Supracoralline beds, like the far-off coral-
liferous deposits at Novion; and it corresponds with the uppermost
portion of the Corallian of the Charente, as described by Coquand.
At the cliff near Angoulins, very little to the south of the Point du
Ché, the last of the rubbly limestones, with Lima leviuscula and
Ostrea cf. gregaria, is seen occupying the base, overlain by about
5 feet of marly beds with Pholadomya Prote: and Ceromya ecacen-
trica of large size, and then a hard limestone band with many fossils,
amongst which are corals, Pecten striatus, and Cidaris Smithir?,
but aiso a great abundance of Terebratula Leymerw. The presence
of this last species would indicate Astartian beds, which are other-
Wise unrecognized; and these are doubtless the beds to which Co-
quand alludes when he says d’Orbigny has placed them with the
Corallian on account of their being calcareous. As noted, however,
by Hébert (54) only nine of the species found here are common to
the Corallian beds at the Point des Minimes. In the same paper we
learn that the marls of Chatelaillon, which show the upper succes-
Q.J.G.S. No. 148. 20
546 J. F, BLAKE ON THE UPPER
sion, contain Amm. cymodoce, Natica hemispherica, Pteroceras ocean,
P. Ponti, Mytilus jwrensis, Ceromya excentrica, Thracia suprajurensis,
and Pinnigena Sausswret, and are therefore very fair represen-
tatives of Pterocerian beds, especially when compared with those at
Havre. Neither these beds nor the overlying Virgulian marls could
be specially examined.
The so-called Portland beds, however, of the Ile d’Oléron demand
particular attention. As in the Charente department, the upper
part is gypseous ; but M. Manes does not on that account call them
Purbeck, but classes all with the Portland. The beds are well dis-
played along the cliffs and shore of the island on either side of the
harbour of St. Denis. The lowest beds seen are (1) massive blue
cale grits, which stand out as reefs at low tide on the north of the
harbour, and are broken up and stacked on the roads. These contain
Ammonites Gravesianus and Trigonia ef. concentrica. They are suc-
ceeded by many other beds, forming scars, which are better seen on
the south of the harbour, though the succession may not be perfect.
The lowest beds seen here are (2) marly limestones and grits, of
unknown thickness, more than 4 feet; next is (3) blue sandy marl,
3 feet; (4) hard blue sandy beds, with circular fucoid markings,
with Mytilus Morrisu, Trigonia concentrica?, Cardiwm morinicum,
and Haogyra nana, 2 feet; (5) earthy marls, 1 foot; (6) solid cal-
careous block, with Cyprina Brongniart (broad var.), Lucina port-
landica ?, Pecten suprajurensis, P. jarnacensis, Cardiwm dissimile, and
Astarte rugosa?, 1 foot; (7) alternations of limestones with luma-
chelles of Hwogyra nana and earthy beds with Cardiwn Morriseum,
6 feet; (8) thin-bedded limestones, with shale and clay, 10 feet.
In the cliffs on the north side, separated from the low-water rocks
by masses of blown sand, are beds which must succeed the above,
but perhaps not immediately. These are (9) alternations of thin-
bedded limestones and black sandy marls, with gypsum, possibly the
continuation of (8), 12 feet; (10) black and white sandy elays, no
fossils, 20 feet; (11) thin-bedded and laminated clays, 34 feet;
(12) black laminated clay and sandy limestones, 8 feet ; (13) purple
lithographic suboolitic limestones in thin beds, the uppermost when
weathered becoming a vacuolar oolite, and containing masses of
shell-fragments, all undistinguishable, unless one is a flattened
_ Cardium dissimite?, 2 feet. Above this are still some white chalky
fragments; but no more is seen. Here, again, therefore the same
argument holds as for the neighbourhood of Jarnac. The fossili-
ferous beds cannot be lower than the zone of Cyprina Brongmart :
and the higher beds must in all probability represent true Portland
rocks. The occurrence of Cardium dissimile is especially note-
worthy. It is found near the top of the series; and in no other
locality does it occur lower than the true Portland. If the rocks
which contain it be of such an age, we must place the overlying
eypseous beds in the same category, unless we choose to call
them Purbeck. This we should not be justified in doing un- .
less we had the whole of the Portland limestone here, which is
improbable.
JURASSIC OF THE PARIS BASIN. 547
II. Normanby witH ORNE AND SARTHE.
1. Department of the Orne and Sarthe.—It has not been possible to
examine the feeble development of the Upper Jurassic rocks in the
narrow strip which leads northwards from Le Mans to Normandy.
We may note, however, that Hébert (21) shows that the Oxfordian
beds with Amm. perarmatus and A. cordatus, which he calls “‘ Middle
Oxfordian,” consist of sand and calcareous grits; while the “‘ Upper
Oxfordian,” with Zrigonia perlata (?‘ clavellata”), Pholadomya de-
cemcostata, Perna mytilordes, and Gervillia aviculoides, is marly. This
is a succession very like that to be seen near Trouville. Near Bel-
léme are said to be seen, over this, calcareous grits full of Trigonia
Bronnw (surely not the Supracoralline species!); next some oolitic
limestones, with large Astarte mysa(?=A. ovalis). Next come piso-
lites with Nerinee (vrobably equivalent to the limestones of Trou-
ville and Osmington); and finally, at some distance above, come
Diceras-beds, containing Cardium corallinum and Corbis gigantea,
which have not been matched further north. These Diceras-beds
elsewhere in the neighbourhood are said to be covered by an oolitic
coral-limestone, very irregular on its surface. This is succeeded by
marls and marly iimestones, with Ostreu deltoidea and several other
of the lower fossils of Havre, such as Trigonia Meriani (“‘muricata”’),
Cyprina cornuta, and Rhynchonella inconstans (?); and after a very
slight interval come the Virgulian marls. These facts are very in-
structive, as showing, amidst a general development similar to that
of Normandy, some of the peculiar features, e. g. the Diceras-beds,
of the great southern range.
2. Normandy.—In studying this district it will be well to go, in
the first instance, to the coast, because there the section is complete
and has been described by several authors. The earliest description
was that by Caumont (1), who gives some account also of the inte-
rior, and recognizes the following subdivisions :—(1) Kimmeridge
Clay, (2) Glos sand and Blangy limestone, (3) Coral Rag, (4) Oxford
Clay. A later and more complete description of the coast only is by
Hébert (28), who gives very detailed sections, and divides the rocks
studied into (1) Coral Rag, (2) Upper Oxfordian, and (3) Middle
Oxfordian. A further description of the higher rocks was promised
at the time, but has never yet seen the light. The continuation
of the series on the opposite side of the Seine, at the Cap de la
Héye, has been described by Dollfus (30), who recognizes three
portions of the Kimmeridgian, as (1) Ammonite-clays, (2) Pteroceras-
marls, (8) Trigonia-clays and limestones ; and by Lennier (49), who
gives a detailed section of the beds at the Cap de la Héve, and
thence to Octéville.
In the examination of this section the English geologist is at
once struck with the extraordinary resemblance of the series to those
at Weymouth and Osmington. So close indeed is it, that almost bed
for bed can be recognized ; and the whole becomes therefore an admi-
rable term of comparison between the French and English rocks,
202
J. F. BLAKE ON THE UPPER
548
oar
ge paps
A
ieee
LU POL
C000
¢
08 : T T8909)
“9p U0noat], wou ysn0g 243 fo dvyy—FT Su
Be es Pow
=
JURASSIC OF THE PARIS BASIN. 549
if only the development in each country could be correlated respec-
tively with these.
The cliffs of Auberville are mainly composed of fossiliferous Oxford
Clay (known as Argile de Dives); and Caumont’s section, in which he
indicates the presence of Coral Rag, Upper Calcareous Grit, and Kim-
meridgeClay beneath the Cretaceous rocks, is quite deceptive. Hébert,
however, gives details of 33 beds seen in the central portion of the cliff,
all referred by him to the Middle Oxfordian. His lower 19 divisions,
comprising 195 feet of clays, with various bands of nodules, would
correspond to the Weymouth Oxford Clay. To within 60 feet of the
top this is pure clay, and bands towards the base are very fossiliferous,
the horizon being indicated by such fossils as Amm. Lamberti, A.
arduennensis, Turbo Meriani, Modiola imbricata, Nucula ornata, and
Tthynchonella varians. These are succeeded by numerous bands of
ferruginous oolite, scattered in the midst of the clays through a
thickness of about 20 feet, after which the clay still continues for
another 40 feet. The whole of these have Ostrea dilatata in great
abundance. One might be tempted to regard the ferruginous bands
as corresponding to the Nothe grits; but the latter are better
represented by the mass which succeeds the Oxford Clay. This
commences with a bed of oolitic grit of about 5 feet, then more
clay for 5 feet, and then 12 feet of strong ferruginous oolite and
grit, which is marly in parts, and has a lumachelle of small oysters
at the top. ‘These beds are very constant: they may be traced
all along the cliff of Auberville as far as Villers, and may be seen
again at low tide on the shore east of Trouville. At this last
locality the lower beds contain Ammonites plicatilis? and Pecten
jfibrosus. ‘The intervening clays make no show; and the upper part
are dark-brown oolitic grits, exactly similar to those at Osmington,
erowded with large Gervillia aviculoides, Trigonia perlata, and
Pecten fibrosus ; towards the top is a bed of Serpula tricarinata,
and, finally, a regular Trigonia-bed like the lower one at Osmington.
These are the beds Nos. 20-29 of Hébert’s Auberville section, and
Nos. 2 and 3 of his Trouville section, which is rather differently
described. The principal fossils noticed, besides those mentioned,
were Astarte ovalis, Cerithium muricatum?, Unicardium globosun,
Pleuromya tellina, and Hxogyra spwralis. The next portion of the
series corresponds to the Nothe clays. It consists at Auberville of
blue clay at the base with hard bands and fossils, and at the top of
purple unfossiliferous clay, making a total of 6—8 feet. At Trouville
the base is darker, and contains lumachelles of Hwogyra nana. There
is a hard blue cale-grit with fucoidal marks at the top, which, from its
position, may be taken as the representative of the Bencliff calc-grit.
These are Nos. 30-32 of Hebert’s Auberville section, and apparently
No. 3of his Trouville section, though the grit is not noticed. Above
these come about 6 feet of alternations of clays and ferruginous oolitic
bands at Trouville, scarcely recognizable at Auberville, in which
Exogyra nana and Pecten fibrosus are still abundant, with Trigonia
corallina, Pecten lens, Lucina Moreana, and Pseudodiadema sp.
These must be reckoned with the succeeding beds, which are perfect
550 ; J. F. BLAKE ON THE UPPER
representatives of the Osmington volites. Like these same oolites
as seen at Weymouth and Osmington, they are in one place more
compact than in another. They are large-grained and more or less
rubbly at Trouville, especially towards the base, and in alternating
bands up to the top, where they are capped by a pisolite full of Verinee,
forming a very characteristic horizon. At Auberville they are like-
wise very oolitic towards the base, and this is the only part of them
which is anywhere seen in the cliff; but as they have a dip towards the
S.E., the upper portion 1s exposed in stream- and road-sections near
Villers, beneath the Cretaceous strata, andis seen to consist of a fine
massive oolite, perhaps as much as 20 feet in thickness, with scarcely
any fossils except Pecten qualicosta. The more pisolitic beds, however,
are crowded with fossils everywhere, the most abundant species being
Echinobrissus scutatus, Opis Phillips, and Cerithium mwricatwn.
Other fossils are Chemnitzia heddingtonensis, Pleuromya Voltzia,
Nerinea elongata (or ? fascrata), Phasianella Buvigmert, and Lima
subantiquata. Above this, at Hennecqville, are seen blackish oolitic
beds, of no great thickness, alternately hard and soft, with Trigonia
clavellata and Gervillia aviculordes, which may he paralleled with
the Trigonia-beds of Weymouth. ‘The series above is variable, as
usual with the Coral Rag. At Hennecqville there are 18 feet of dark
unfossiliferous clay, rather sandy at the top, and rapidly changing in
character towards Trouville, where it is almost concealed. Hébert
mentions that at Villers, in some locality which is now imaccessible
to observation, marls and limestones with Ctdaris florigemma succeed
the oolites. Above this clay at Hennecqville the beds become oolitic
again through 12 feet, and very similar to those below*, most fer-
ruginous at the base, and cavitary towards the top by the decay of
fossils, the most abundant of which here are Opis corallina and
Nerinea fasciata?. There are also Cerithium muricatum, Littorina
murieata,and [sodonta Deshayesia. The capping of this mass for about
1 foot at Hennecqville is a ferruginous suboolitic limestone, full of
fossils, especially Cedaris florigemma and some corals—also Nerina
imbricata, Opis corallina, Cypricardia isocardina, Pleuromya tellina,
Pecten vinmneus, P. qualicosta, Lima proboscidea, Exogyra nana, &e.
This is the only representative of Coral Rag at this spot, where the
clay is thick; but as we pass towards Trouville all that hes above
the Osmington Oolite rapidly changes its character and becomes more
calcareous. ‘The last exposure fomande the town shows massive lime-
stones with rubbly Ovdaris-florigemma beds towards the top, through
an aggregate thickness quite as great as at Hennecqville (31 feet) ;
and in a large quarry in the town are seen beds which must be the
representatives of this portion, though very dissimilar. Here at the
top is a rubbly coral-reef mass, utterly irregular atits base, lying in
* This clay and oolite are so similar to the clay and oolite below, that it is
possible one may be deceived by slips, and they may be actual repetitions. At
no place can the beds above the Lower Oolite be certainly determined ; but at
Trouville they actually lie at a considerable depth below the beds saith Cidaris
florigemma, which latter are underlain by a more compact limestone. If there
be a slip, it is a very uniform one and ‘parallel to the face of the cliff.
JURASSIC OF THE PARIS BASIN. 551
ereat depressions of the subjacent limestones, and at places 20 feet
thick. ‘The corals are Thamnastrea and Calamophyllia ; and Crdaris
florigemma and C. Smithw also abound, with Littorima muricata,
Pseudomelania Coquandi?, Natica corallina, Pholadomya Tombecki,
Corbicella sp., Ostrea gregaria, and Acrosalena sp. Underlying
this are 20 feet of shelly oolites, in which the fossils are badly pre-
served, Trigona corallina(?) and Opis corallina being the chief noted.
Below these again are 4 feet of rubble (with Hinnites velatus), and
then 3 feet of oolite. This quarry does not appear to have been de-
scribed before ; but it is of considerable importance as showing the
rapid development of coral-growth, since, not a mile away, only the
feeblest representative is seen in the cliff. In the other direction,
towards Auberville, however, it becomes perhaps of still greater im-
portance ; for at Benerville admirable coral-masses are developed, and
slip down onto the sea-shore. These are of considerable thickness,
and contain a crowd of all the usual Rag fossils, as at Trouville; they
are underlain by oolitic stone and unfossiliferous clay. The whole
mass, however, is out of place; and no stratigraphical data are obtain-
able. Hébert does not notice this, though he describes the clay
onto which it has slipped as crowded with Oxfordian fossils. At
Villers only fragments are now visible; and, according to Heébert’s
section, the reef is dying out; for he indicates only about 16 feet
of limestones and marls, including the florigemma-rag. From the
position which this rag occupies with relation to the beds below, and,
as will be seen, to the beds above also, it follows that it occupies the
place of the “ Sandsfoot Clay,” and possibly of the lowest bed also of
the “‘ Sandsfoot Grit,’ many of the fossils of which are common to it.
It is, however, so intimately connected with the subjacent oolites, as
to make it difficult to range the two in different subdivisions of the
geological series.
Above the representative of the Coral Rag at Hennecqville, where
alone any higher beds are seen on the coast, come calcareous grits
and sands, admirably representing (as will be seen) the Sandsfoot-
Castle beds. For the lower 15 feet they are marly sandstones with
Pseudomelania striata and a narrow Nerinca; then comes a hard
calcareous grit, called by Caumont the Blangy lmestone, from its
being worked at a village of that name; and above this a series of
beds varying very much in thickness, containing, towards the base,
white hummocky calcareous grits with intervening yellow sand and
beds of Tregonia muricata ; then fucoidal grits and sands, with great
masses of black flints, dying out to nothing (one was noticed 3 feet
thick by 16 feet long); and at the top honeycombed masses of soft
and hard sandy beds, the cap being especially hard, and serving as
a ledge on which the overlying clay appears to rest conformably,
though it has doubtless slipped down and covered the intervening
beds seen further east at Villerville, and blocks of which here strew
the strand. The whole thickness of these is nearly 40 feet; and
they contain also Ammonites varicostatus, Chemnitzia delia, and
Pinna granulata.
So far the section, instructive both by its resemblances and by
Ou
52 J. F. BLAKE ON THE UPPER
its differences when compared with that at Weymouth, has been
described before; but the succeeding beds which connect it with
the section at Havre, and complete the similarity of the whole
to the English series, appear to have escaped description. So com-
pletely, indeed, have they done so that Hébert (see 41) states that
the Trigonia-grits of Havre are separated from the base of the
Kimmeridge Clay by 160 feet of marls which overlie the Corallian
beds at Hennecqville, these 160 feet being obviously the overlying
clays which have slipped forward and covered the grits which are
seen i sitw further on. Though of considerable thickness, they
have been subjected to so much disturbance that they make but
little show even when exposed, as on the shore on either side
of the village of Villerville. First, overlying the last-named grit of
the Corallian series, which forms an admirable base line, are about
8 feet of marls; and next a series of remarkable hard beds filled
with small shells. These extend through about 4 feet, and are
flaggy; some of the bands are crowded with a small Cerithium ;
others have abundance of Astarte supracorallina, Cardium deli-
batum?, and Haoyyra bruntrutana. Next come perhaps 10 feet
(more or less) of grey marls; over which lies, apparently an situ, a
gritty bed full of black pebbles; then more marls, 8 feet to 10 feet ;
and finally, in this locality, 3 feet 6 inches of oolitie ironstone
and associated marls with Pecten midas. Allthese are seen together
to the west of Villerville. On the east side, presumably the same
oolitic ironstone bands are seen in slipped masses on the strand,
followed in an upward direction by flaggy sandy marls full of
Pleuromya Volizi; then some more marls, 8 feet; next a bed of
small oysters (Hvogyra nana or bruntrutana), 1 foot; next 3 feet of
soft marl; and then the remarkable sandy grit with Tragome, so
well known at Havre and Weymouth, about 1 foot in thickness ;
above which come about 4 feet of clays with two bands almost made
of O. deltoidea; and finally the ordinary completely argillaceous
Kimmeridge Clay, which so often slips down and masks the beds just
described. If any one compares this section with that at Sandsfoot*,
he will see an almost exact identity, in which the ironstone, the
lumachelle, and the Trigonia-grits hold their relative positions and
almost their distances—the only difference being that the O.-deltoidea
beds appear here to lie, as they are said to do at Havre, above the
Trigonia-erits instead of below. ‘The fossils also are equally charac-
teristic, those noted being Ammonites cymodoce, Belemnites mtidus,
Inttorinma pulcherrima, Natica eudora, Pholadomya “ Protet,” Opis
angulosa, Astarte Michaudiana (called ovata before), A. trigonarun,
Cyprina Constantin, Cyprina cyreniforms?, Trigoma Meriani,
I’. muricata, T. papillata, Mytilus peetinatus, Pecten midas, P. swpra-
jurensis, P. minerva, Gervillia kimmeridiensis, Serpula gordialis, S.
qunquangularis, S. tetragona, and Monilivaltia Lesueurn. The pre-
sence of this latter fossil 1s of interest as showing that coral-growth
had not died out here; for it must be to the lower portion of this
series that the ‘“ Upper Coral Rag” seen in Ringstead Bay must be
* Q. J. G.S. vol. xxx. p. 241, and vol. xxxili. p. 270.
JURASSIC OF THE PARIS BASIN. aes
referred, which is, at the same time, proved to be on a much higher
horizon than the ordinary Coral Rag of Normandy.
The section thus concluded at Villerville can be perfectly taken
up on the other side of the estuary at Havre; for the “ Trigonia-
erit” at the former is simply the continuation of the “ Calcaire a
Trigonies” at the latter, of which the fauna has been so admirably
illustrated by Dollfus. ‘These, including the associated marls and
other hard bands, up to and including the grey clay over the fossili-
ferous grit, are therefore the Kimmeridge passage-beds, as was
ascertained by Waagen (35). Itis also obvious-that by their stra-
tigraphical position and by many of their fossils they represent the
Astartian beds of the rest of France *. Of the overlying beds at
Havre little need be said, since their position cannot be otherwise
than clear. ‘The beds included between No. 4 and No. 14 of Len-
nier's section, the latter being a hard band with many gasteropods,
represent Dollfus’s “* Marne a Pteroceres,”’ and the basal portion of
the Lower Kimmeridge of Weymouth. In Normandy there is
certainly much more reason for establishing a “ Pterocerian stage,”
since Pteroceras Ponti is a very common fossil both at Villerville
and at Havre, and has associated with it a sufficiently distinct
fauna. It is therefore perhaps only due to the imperfect searching
of the beds at Weymouth that a similar fauna has not been dis-
covered there. Of the fossils in Dollfus’s list which are found only in
the Pterocerian beds, the following occur in the Lower Kimmeridge
of Weymouth—dAmm. decipiens, Pleuromya tellina, P. donacina,
Pholadomya acuticosta, and Ostrea solitaria. Only one of these is
at all characteristic ; and that is Phol. acuticosta, which, as we have
seen, is a constant species in the Virgulian marls, whether these are
divisible into two parts or not. In fact the fauna consists almost
exclusively of Myacidze, Gasteropods, and Echinoderms, of which
the latter two groups are so remarkable tbat they could scarcely
escape attention if they occurred at all freely at Weymouth. Hence
though the beds must correspond stratigraphically, we have no en-
couragement in this country to recognize a ** Pterocerian” subdivision.
Two other fossils may be noted. Avicula edilignensis occurs in these
beds, which may hence be a guide to correlation: and about halfway
between the Trigonia-grits and the Gasteropod-bed are bands full of
Terebratula Leymeru, with associated nodular beds. It would
therefore be perfectly defensible to raise the upper limit of the
Astartian to this level, except that 4. virgula has already begun to
be abundant. The “ Ammonite clays” of Dollfus present no points
of interest, as they are but poorly seen and slightly fossiliferous, and
they do not attain to the Upper Kimmeridge.
The only other locality examined in Normandy is the neighbour-
hood of Lisieux and Glos, which presents us with a greater develop-
ment of a portion of the series seen at Trouville. This locality is
included in the general description of Normandy by Caumont, who
* This is not the conclusion I arrived at in my paper on the Kimmeridge
clay ; and the correction shows the advantage of a personal over a literary
acquaintance with the French series.
554 J. F, BLAKE ON THE UPPER
gives a section of the hill of Glos; and it is specially described by
Goubert (29), who, with Zittel, illustrated the fossils found in the
sands. Near Lisieux, on the road to Glos, is a quarry very similar
to that at Trouville; for at the base is 6 feet of rubbly limestone,
then 5 feet of a large-grained oolite, and on the top 20 feet of rubbly
coral rag, almost a Thamnastrean reef in places, and containing
Cidaris florigemma abundantly. This, therefore, represents the
true Coral Rag. At a distance of about 3 kilom. from this quarry,
on the north side of the bridge leading to Glos, is a very instructive
exposure. At the base we have a rubbly coral rag of different
character, and obviously either overlying the former, or a changed
development of its upper part. ‘The beds are all vacuous by
the decay of fossils, only internal and external casts being found.
The corals are Calamophyllian, and not Thamnastrean: and there
is an abundance of Nernea Goodhallu, with Littorina muricata,
Cerithium muricatum, Trochotoma discoidea, Chemntza dera?,
Natica corallina, Nerita sp., Lucina Moreana, and L. balmensis?
The whole, by the absence or rarity of Cidaris florigemma, by the
abundance of Nerinewe, and by the character of the corals, reminds
one of the Novion hmestone, though the lithology is different. Over-
lying this are oolites and oolitic sands in good beds, 34 feet; next a
breccia of limestone-fragments with a hard 15-inch band of blue
limestone in the middle, with Plewromya tellina, a total of 3 feet
9 inches; and then the true sands of Glos. These are marly at the
base, but become more sandy by degrees, with hard glauconitic
bands or nodules containing fossils; but finally the sand is abso-
lutely unfossiliferous, as it has usually been reported to be at this
spot. The thickness here seen is 24 feet; but it certainly extends
much further up the hill. The fossils noted are Ammonites serratus,
Pterocera polypoda, Trigoma Brenna, Gervillia kimmeridiensis,
and Pecten midas—a group rather characteristic of higher beds
than these are usually considered, and which leads us to look on
these sands as partly equivalent to the passage-beds of the coast,
especially as Caumont records a section at Pont l’Evéque where the
Trigonia-grit les immediately on the sands of Glos. The quarry
just described does not appear to be the place where the usual fossils
have been gathered, as they are said to be all small except the
Trigonia. The common locality in fact is seen on the opposite side
of the river, where a greater thickness of sand is seen containing
bands white with fossils, the principal of which are Trigonia Bronnw
and Lucina circumcisa. In any case, the exact position at which
the sands commence in reference to the coast-section is clear, the
lower beds in the quarry representing the first beds above the Coral
Rag, and the blue lmestone the hard band (called ‘Calcaire de
Blangy’’) in the Hennecqville Chiff.
IV. Tue Pays bE Bray.
The older works on this district, such as that of Graves (8), have
been rendered out of date by the splendid monograph of M.de Lap-
JURASSIC OF THE PARIS BASIN. 555
parent (69), published as one of the memoirs of the Geological
Survey of France. Only a small portion of the Upper Jurassic
rocks is exposed in this district, brought up to day by a N.W.
and S.E. elevation, from the summit of which the Cretaceous rocks
have been worn away. It thus affords, as it were, a continuation
of the coast-section of Normandy, commencing at the base where the
latter ceases, namely in the Virgulian marls. M. de Lapparent
classifies the rocks thus exposed as follows :-—
Upper PorTnanp.
Ferruginous sandstone, speckled clays, greensand.
Mippie Portuannd.
Blue marls.
LOWER PorTLAND.
1, Upper conglomerate.
2. Glauconitic calcareous grit.
3. Marly limestones.
4. Calcareous grit with Anomie.
5. Beds with Ostrea catalaunica.
KIMMERIDGIAN.
1. Upper clays and lumachelles.
2. Compact lithographic limestone.
3. Lower clays and lumachelles.
4, Calcareous grit (Pterocerian or Astartian ?).
The accuracy of this description has been verified so far as may be
in a brief visit, and the correctness of the correlation determined—
with one important exception, which may be the subject of discus-
sion. According to verbal communications from M. de Lapparent,
borings executed between the Pays-de-Bray and Boulogne have
shown Cretaceous rocks lying directly on Paleeozoic ; so that we are
not led to expect the Jurassic rocks to be continuous between the
two districts. Nevertheless, as we have seen, the lower portions of
the deposits under study are remarkably similar to those of England ;
and as the true Portland rock of England reaches to Boulogne with
little change, we may expect the intermediate beds to be also similar
to those of England and differing from them in the direction of
Bolonian characters. Judged in this way, the so-called “ Lower
Portland” (used in the Bolonian sense) of the Pays-de-Bray should
begin to show its episodal character somewhat lower in the series.
The lowest bed visible, the sandy calcareous grit, is a very
doubtful rock, seen only at one place. One cannot be sure that it is
im situ; and its badly preserved Trigonie and Astartw suggest that it
may be a mass belonging to No. 3 of the “ Kimmeridgian.” In any
ease it has no particular resemblance to the Trigonia-grit of Havre,
and cannot lead to the inference that we are here low down in the
Kimmeridgian, as we should be if it belonged to the “ Pterocerian
or Astartian.” The ‘‘ Lower Clays and lumachelles” with Kwogyra
virgula present nothing worthy of note, except that towards the
south they have a thickness of 200 feet, and on the opposite side of
the same valley between Louvicamp and Mesnil, which contains the
556 J. F. BLAKE ON THE UPPER
Fig. 15.—Map of Part of the Pays de Bray. (Scale 1: 240,000.)
¢ See . Zam Sn
5 Sree ) SS ;
fim Cay). LE EX
ya ae 5
grit above discussed, they are not much thinner. The upper portion of
this, in which the lumachelles and the intervening material become
very sandy, requires more discussion. M.de Lapparent says :—“ At
the top of this system the lumachelles grow together into solid banks
intercalated with very sandy material, and forming rather irregular
masses than continuous beds.” ‘These sands and doggers are well
i! seen to the north of Louvicamp. The sand is pure; and the doggers
i are huge; and at the top is a lumachelle of Trigonie, which appear
| to be 7’. Muniert. We have therefore the exact representative of the
if sandy beds at Gris Nez and Mt. Lambert in the Boulogne area. The
li same is exposed in the railway-cutting south of Haussez, where the
beds seen are 10 feet or 12 feet of grits and sands, thickening to the
south, and with abundance of Hwvogyra virgula. ‘The presence of this
last fossil may at first appear a stumbling-block; and it undoubtedly
proves the close connexion of these rocks with the Virgulian; yet,
when we compare the Boulogne district, it proves nothing, since the
| species is equally abundant in the sandy beds which in that area are
iy referred to the “Lower Portland;” on the other hand the petrological
ir similarity is of great weight. Overlying these comes the ‘Compact
hy Lithographic Limestone,” a rock which can be scarcely be matched
either in England or at Boulogne. It has a thickness of certainly
more than 12 feet, and contains lumachelles of Trigonie too deeply
imbedded for the species to be recorded. At Louvicamp it has also
lumachelles of Kxvogyra virgula. The two fossils mentioned by M. de
Lapparent are Ammonites cf. gigas, too characteristic a fossil to be mis-
taken, and Gervilla kimmeridiensis, which might well be G. linearss,
so similar are the species of this genus. Next comes another mass of
clays which are said to be likewise 200 feet thick in the south, but are
Ad certainly not so much in the central portion, where examined. There
abs are few fossils in them beyond Lwogyra virgula, which occurs in luma-
: chelles. It is seen underlying the cement-stone beds of the cutting
at the station of Saumont-la-poterie. These cement-stones are
regarded by M. de Lapparent as forming the base of the ‘‘ Lower
Portlandian ;” and he states that Hwogyra virgula is entirely and
suddenly replaced in them by Kw. catalaunica. ‘This is certainly
A not the case: after the cement-stones begin there are no more
lumachelles; but Ha. virgula occurs in tolerable abundance in the
marls above, at least 6 feet of them. ‘This fossil, therefore, is no
more available here for drawing a line at the base of the ‘‘ Lower
~
JURASSIC OF THE PARIS BASIN. 557
Portland” than itis at Boulogne. The fossils of these cement-stones
are abundant; they are Ammonites swprajurensis, Natica athleta?,
Pleuromya stnuosa, Thracia incerta, Cyprina elongata, C. implicata ?,
Trigonia (clavellate sp.), Mytilus autissiodorensis, and Anomia lavi-
gata. The lithological character of these limestones, and the abun-
dance of Mytilus autissiodorensis and of T'hracia incerta, lead one in
the first instance to recognize in these beds the cement-stones at the
base of the Portland sands; but in face of the abundance of Ex. vir-
gula and the presence of Amm. suprajurensis, it is safer to look upon
these as the more marly portions of the “ Lower Portlandian,” such
as are associated with the conglomerates at Portel and are abundant
with the same fossils in Kimmeridge Bay. These cement-stones
are cut off from less fossiliferous marly beds above by an inter-
mediate bed of “ Calcareous Grits with Anomie.” These two, with
the ‘‘ Glauconitic Calcareous Grit” and ‘‘ Upper Conglomerate” form-
ing the cap, will then represent the uppermost portion of the Bolonian
“¢ Lower Portland ” with Pteroceras oceant. That fossil is not recorded
from the Pays de Bray; but the occurrence of Trigonia boloniensis,
Pecten nudus, and a Hemeidaris called H. Hofmanni, but perhaps
really H. purbeckensis, is highly characteristic. Of the upper beds
little is now visible. The blue marls, described by de Lapparent as
dark at the base, with Cardiwm morinicum and large Ammonites
(? biplex), and calcareous towards the top, with Amm. biplea, Pleu-
rotomaria Rozeti, Ostrea expansa, Perna Bouchardi, and Cardium
Pellati, are obviously representatives of the ‘“‘ Middle Portland” beds
of Boulogne, and are more similar to them than to the corresponding
English series. Finally the ferruginous sands seen at Gournay are
certainly distinct in appearance from any thing seen elsewhere: and
they contain few if any fossils. At their base, however, they contain
huge calcareous-grit doggers, which resemble very much those of
Swindon and Shotover, the corresponding beds at Boulogne being
more regular and calcareous. These contain clavellate Trigonie,
Astarte, Corbula, and Thracia incerta? It is above these beds that
ferruginous nodules are found, which contain Trigonia gibbosa and
other true Portlandian Trigome, e. g. T. oncurva, the specimens of
which from the Normanville cutting, near Gaillefontaine, preserved
in the Ecole des Mines at Paris, are undoubtedly the true forms,
though they can no longer be found in a recognizable state. While,
therefore, the lower part of the sands and grits may well be the
equivalents of our “ Portland Sands,” the upper part must at least
attain the horizon of the Flinty series of Portland.
V. Tue Bovunonnals.
The coast of this district is almost English ground: so well is it
known, and so long has it been studied by many of our native geolo-
gists. They have, however, published little upon it; and we owe the —
description of the area first to M. Rigaux (33) and Prof. Hébert
(37), and later to MM. de Loriol and Pellat (86, 39, 41, 56, 61),
the last-named author having given a final réswmé of his views in
1878 (68). M. Pellat’s classification is now as follows :—
508
J. F. BLAKE ON THE UPPER
Urrrer Portnuann.
. Cypris-beds, 25 metres.
. Siliceous limestone with Cardiwm dissimile, 24 m
. Sands and grits with Natica elegans &e., 4 m.
. Sands and cale-grits with Cardiwm Pellati, 3m.
MippLE Portnanp.
O,. Clays and glauconitic limestones with Ostrea expansa, 13 m.
O,. Clays with Cardiwm morinicum, 15 m.
Lowrr Portianp.
Zone of Cyprina Brongniarte.
N,. Sandstones with Preroceras oceani 10
N,. Sands with Nautica Marcousana a
N,. Conglomerate with Trigonia Pellati of Chatillon.
Zone of Ammonites gigas.
N,. Sands and grits with Amm. portlandicus, '7 m.
M,. Shales and upper cale-grits with Hemicidaris purbeckensis, 17 m.
Upper KIMMERIDGIAN.
Zone of Anvmonites erinus.
M,. Shale and lower limestones with Amm. erinus, 12 m.
L. Sands and grits with Pygurus, 43 m.
Mipp.ie KIMMERIDGIAN.
Zone of Ammonites caletanus.
Clays and upper lhmestones with Amm. caletanus, 18 m.
. Sands and grits of Conincthun, 2 m.
aia
Lower KIMMERIDGIAN.
Zone of Ammonites orthoceras.
I. Clays and lower limestone with Amm. orthoceras, 22 m.
H. 138 beds and little beds of Bréqueréque, 15 m.
SEQUANIAN.
G. Sands and grits of Wirvigne, 5 m.
F,. White marls and oolites of Bellebrune, 4 m.
. Clays with Ostrea deltoidea, 2 m.
. Pisolite with large Nertne@e of Hesdin-l Abbé, 6m.
E. Red limestone, sands and grits, with Triégonia Bronnii, 5 m.
D. Clays with O. deltoidea of Brucdale and Mont des Boucards, 10 m.
CorRALLIAN.
A'. Coral Rag with Cidaris florigemma of Brucdale.
Limestones of Mont des Bou-
cards = Pyritous claysand lime-
stones of the South of the Bou-
lonnais, 50 m.
Limestones with J/socardia.
. Limestones with Jerebratule.
. Coral Rag with Cid. florigemma.
HO
Upper OXxForDIAN,
Houllefort limestone with Psewdomelania heddingtonensis, 1 m.
Clays with Ammonites Martelli and sponges, 14 m.
Mippue OxrorDiANn.
Clays and limestones with Ostrea dilatata, 5 m.
Black clays of Wast, 6 m.
Lower Oxrorp1An (Callovian).
Fissile limestones with Ammonites Lamberti, 2 m.
Clays with Ammonites Duncani, 6 m.
Ferruginous clays with Ammonites calloviensis, 5 m.
ee
JURASSIC OF THE PARIS BASIN. 559
This classification is the result of several modifications of pre-
vious ones, especially in the matter of names.
The Upper Jurassic strata in the Boulogne area lie in an anti-
clinal whose crest has a slope from E.N.E. to W.S.W. Hence the
Fig. 16.—Map of Part of the Boulonnais. (Scale 1: 240,000.)
Zz
argunse
OW. Bein ehurs
lowest strata are seen in the E.N.E. corner, and the succession may
be traced by passing thence to the sea at Boulogne, whence a diver-
gence to the right or left will show the uppermost portions. The
development is also greater towards the 8.W., as in the contrary
direction we approach the shore-line. From M. Pellat’s beds E.,
or the base of the Nerineean limestones, downwards, the prevail-
ing character is argillaceous, and the comparatively feeble lime-
stones are merely intercalated masses, themselves usually more or
less marly. This feature renders the correlation somewhat difficult,
and has given rise to the complicated classifications of MM. Pellat
and Rigaux.
The lower groups of clays, estimated by M. Pellat at 26 metres
in the north, but at 47 metres in the south-west, have not been spe-
cially examined. The uppermost portion, with dAmm. cordatus and
Millericrinus, doubtless corresponds to the Nothe grits and clays, and
560 J. F. BLAKE ON THE UPPER
to the beds with Trigonia spinifera at Neuvizy, and with Trigonia
perlata at Trouville. The first mass of importance is the limestone
of Houllefort, which is perfectly isolated in the midst of clays, some of
which separate it above from the so-called limestones of the Mont -
des Boucards*. It is extremely fossiliferous ; but the discovery of
the fossils is dependent on their weathering out, and would be very
unlikely in a boring. ‘Twenty-six species are enumerated by de
Loriol from this limestone, and additional ones by M. Pellat. Those
actually noted were Trochus houllefortensis, Purpura sp., Cerithium
Struckmanni, Chemnitzia sp. (wrongly called Pseudomelania heddingto-
nensis), Opis Phillips, Arca scabrella (near to A. quadrisulea), Nucula
cottaldina, Lama rudis,and Cidaris florigemma. There is so much that
is peculiar about this fauna that it gives little help in correlation; and
the additional known species in de Loriol’s list, ¢. g. Amm. plicatilis,
Alaria tridactyla, Pholadomya Prote and P. concinna, Trigonia moni-
lifera, Lima rignda, Pecten vimineus, and Ostrea dilatata are not quite
conclusive. Nevertheless, on the whole, the facies is Corallian, and
indicates an horizon which may indeed be compared with that of
Neuvizy or the Osmington Oolite, but is more like the base of the
Corallian in the Haute-Marne and the Yonne departments.
About the succeeding portion of the series there have been
several changes of opinion among the French geologists, owing
to there being different developments in different parts of the _
area. The difficulties arising from this are intensified in the
Boulonnais by the deposits being exceedingly local and by several
minor unconformities occurring in the series, owing to the proximity
of the ancient shores. Four localities exhibit different arrange-
ments, of which the sequence may be specially noted. First, in
the extreme north near Bazinghen there is nothing but a few feet
of clay between the Callovian grit with Terebratula humeralis (true)
and Rhynchonella varians and the Nerinewan or so-called Astartian
Oolite; thisisa minimum. Secondly, at the Mont des Boucards, there
is a maximum; but the whole is essentially argillaceous though dig-
nified by the name of limestone. Only at one spot on the hill-side
are seen a large number of loose stones scattered.on so restricted a
surface as to even suggest the question whether they may not be the
débris of ancient buildings. These stones, surrounded on all sides by
the clay, are probably a remanié collection, or are due to some special
cause which renders their actual position, at a slightly lower level than
the fossiliferous beds in situ, of little consequence; but their fauna
is remarkable for its richness and abundance. The list published
and illustrated by de Loriol is very defective, including only twenty-
six out of eighty species which M. Pellat has, up to the present, dis-
covered; and half an hour’s search obtained the following 30,
several of which are not included in de Loriol’s list. Nautilus
giganteus, Aporrhars elegans, A. musca, Pleurotomarva hesione, Ani~
* Tn his later descriptions (e. g. 56) M. Pellat places the “ Calcaire du Mont
des Boucards” immediately above the Houllefort limestone; but in his earlier
ones (e.g. 41) he recognizes that they are separated by a considerable mass of
clay.
JURASSIC OF THE PARIS BASIN. 561
socardia elegans, Trigona monlifera, Arca Sauvage, Cucullea
(called quadrisulca, de Lor.), Arca rhomboidalis, de Lor., Gastro-
chena boucardensis, Nucula equilatera, Astarte Sauvage, A. num-
mus, A. bruta, Lithodomus inclusus (in Isastrea), Modiola cequi-
plicata, Mytilus pectinatus, Inma proboscidea, Pecten vimineus, P.
intertextus, Avicula oxyptera, Plicatula horrida, Exogyra nana,
Osirea rastellaris, Terebratula tetragona?, Rhynchonella corallina,
Thecosmilia sp., Serpula Royert, Cidaris florigemma, C. Smithii, Pen-
tacrinus cingulatus ?. These fossils being collected from the surface-
stones, it is quite possible that some may be derived from overlying
beds, which would account for their only being recorded by de Loriol
as from such. But when we consider also the more important fossils
recorded by him in addition to those above, such as Belemnites nitidus,
Anatina striata, Astarte Michaudiana, Opis Phillipsi, Arca texta,
Hinnites fallax, and Hemicidaris intermedia, we see that there is a
very feeble minority, almost an absence, of Oxfordian species, and that
the whole indicates a higher horizon than the usual florigemma-rag.
If it be a remanié deposit, it might well be formed by the breaking-
up of beds overlying the Coral Rag of Brucdale. The marly beds zn
situ which, with the above exception, continue upwards at the Mont
des Boucards the clays overlying the Opzs-limestone, are well seen
in cuttings and quarries on the hill-side. Only here and there they
have hard bands; and the term “limestones” is quite deceptive.
Only one soft chalky limestone caps the whole, and forms the top of C
of M. Pellat. At the base these beds are crowded with Terebratula
insignis and Rhynchonella corallina (quite a repetition of the chalky
limestones of Bourges), and here and there are lumachelles of Ostrea
nana, and occasional deltoid oysters ; Mytilus pectinatus and Ostrea
solitaria(rastellaris) are also abundant. The other fossils observed are
Ammonites boucardensis [?|, Nucula Menke, Cardium Dufrenoycum,
and Astarte nummus. A total of fifty-one species is recorded from the
basal portion by de Loriol, an examination of which shows the same
tendency as the above, namely to associate these with true Supra-
coralline beds, or at most with the highest part of the Coral Rag, and
to make it difficult to conceive how any one could have taken them
for Oxfordian. The upper portion, C of M. Pellat, is, above all things,
characterized by the presence of Ceromya excentrica, Isocardia striata,
and Mytilus perplicatus, fossils which are everywhere more Astar-
tian than Corallian ; the others noted are Arca rhomboidalis, de Lor.,
Cardiumn intextumn, C. orthogonale, Pleuromya tellina, and Exogyra
bruntutana, which have little effect on the correlation. These marls
are followed by more dark clays till the ferruginous grits are reached.
In the third locality, that of Brucdale and the neighbourhood, are
seen at the base 6 or 8 feet of Coral Rag zn situ, with the Tham-
nastree in their place of growth ; but the whole thickness is not seen,
nor any thing below the Rag. The fauna is an ordinary Rag one, incla-
ding Cidaris florigemma and various Gasteropods and Lime. There is
certainly some difference between it and that of the coral stones of the
Mont des Boucards. ‘This is doubtless largely due to want of search
among the latter; yet what difference there is indicates a higher
Q.J.G.8. No. 148. QP
562 J. F. BLAKE ON THE UPPER
horizon for them than for the Rag of Brucdale; for the fauna of the
Mont des Boucards contains seven species usually found on higher
horizons, and that of Brucdale one only, the species of downward ten-
dency being equally divided. ‘The surface of the Rag of Brucdale is
eroded; and it was doubtless during the interval thus indicated that
the peculiar beds of the Mont des Boucards were deposited, while
the overlying marls spread over both areas. The fourth locality
is the valley of the Liane near Hesdin-l Abbé and at Outreau, where
two borings were made, by which it is supposed to be proved that the
“‘ limestones” of the Mont des Boucards underlie the Rag of Brucdale.
Beneath the latter,it seems, there were encountered some “ limestones”
which were supposed to be identical with (51, 53) those of the Mont
des Boucards ; but when the proofs are examined, these are found to
consist solely in the fact that some shells were brought up which
were thought to be the Ceromya of the Mont des Boucards—a fact
not sufficient, even if the determination were right, to fix the horizon.
No other fossils appear to have been obtained, which is rather extra-
ordinary, considering the great abundance of Terebratula insignis at
the Mont des Boucards. The supposed proof is therefore utterly in-
adequate, and we may with more probability interpret the boring dif-
ferently. At the top (see 51, 53) we have, below the alluvium, 22°65
metres of undisputed beds, down to No. 18; No. 18 is 6-40 metres
of the Nerinzan oolite of Hesdin-l Abbé; No. 19 and part of No. 20
(say 3 metres) are the grits with Trigonia Bronnii. The remainder of
No. 20 are the Ostrea-deltoidea marls, 12:90 metres; Nos. 21-23,
which MM. Sauvage and Rigaux refer to a coralline limestone, though
there are no corals recorded, are attenuated representatives of the
Mont-des-Boucards limestones, not well developed and therefore
without the Terebratula insignis, 4°75 metres. No. 24 is the Coral
Rag of Brucdale with Cidaris florigemma, 6:60 metres. Nos. 25-29,
referred by MM. Sauvage and Rigaux to the Mont-des-Boucards lime-
stones on account of their containing a Ceromya at Hesdin-l’Abbé, are
the marls above the Houllefort limestone, containing Cidaris flori-
gemma and many fragments of fossils; and the poorly characterized
beds below are the ordinary Oxford Clay.
The next bed presents no point for discussion ; itis a ferruginous
erit of little thickness whose characteristic fossils are Trigonia
Bronnit and Astarte communis (Morine). Its place, its fossils, and
its mineral character assimilate it at once to the sands of Glos, the
corresponding beds at Trouville, and the Sandsfoot grits. It is suc-
ceeded by the most constant limestone of this part of the Jurassic
series. Varyingin thickness and somewhat in character, this latter
may nevertheless be easily traced from the extreme north near
Basinghen to the valley of the Liane. Like the others, it begins in
the north by being thin and somewhat sandy, with large-grained
oolites only here and there, and few fossils beyond Terebratula insignis.
It has gained considerable thickness near the Mont des Boucards ;
at Paincthun the oolite predominates, and at Hesdin-l’Abbé forms
thick masses which are extremely fossiliferous, the most noticeable
species being Nerinewa Desvoidyi, N. cecilia, Pholadomya hortulana,
JURASSIC OF THE PARIS BASIN. 563
P. Protei, Ceromya excentrica, Pinna pesolina, Pecten midas, and
Rhynchonella corallina. From this oolite are also recorded Cidaris
florigemma and Hemicidaris intermedia. Ail the more important
fossils except the Pholadomye come up from below and finish in
this bed. It is, however, coloured on the geological map with those
above it as belonging to the “ Astartian.” It is denoted by F’ of M.
Pellat. The succeeding beds F? and F°, are comparatively unfossi-
liferous ; but their fossils are such as would unite them rather to the
overlying than to the underlying beds, Ostrea deltoidea and Trigonia
papillata being the chief recorded. The Grés de Wirvigne, assimi-
lated by M. Pellat to the Trigonia-grits of Havre, is somewhat dif-
ferent from them in mineral character, being more siliceous and full
of oysters; it has a thickness of 6 feet, and is overlain by marly beds
with hard bands. The fossils observed—Ammonites Berryeri?,
Purpura sp., Leda venusta, Astarte supracorallina?, Corbula Des-
hayesea, Trigoma Meriani?, Cyprina cyreniformis, Pleuromya tellina,
Pecten solidus and P. strictus, as well as others recorded, such as
Ammonites erinus, Lucina substriata, L. rugosa, Pinna granulata,
Exogyra virgula, Terebratula subsella, Pygurus Blumenbachii, Rhab-
docidaris Orbignyana—all have a tendency to confirm M. Pellat’s
conclusion ; and scarcely one is more connected with beds below than
with those above. It is possible that these grits and associated
beds represent more than the Trigonia-grits of Havre and Wey-
mouth, since there is nothing above them that can be called Ptero-
cerian. :
The overlying beds, in fact, are seldom seen. On the hill-slopes
south of Mont Lambert but little can be made of them; and the
same is the case in the north, near Bazinghen. At Boulogne they
are hidden beneath the town, and merely a part is exposed at Bréque-
recque, .nd contains no fauna which can be specially called Pteroce-
rian. It is perhaps scarcely worth while to separate these beds from
the overlying ones, called H and I; but we may usefully charac-
terize this lower mass by the presence of Ammonites orthoceras, which
is associated with Thracia depressa, Lucina minuscula, Pholadomya
acuticosta, Arca texta, Gervilia kimmeridiensis?, and Anomia sp.;
it then represents the zone of that Ammonite, and will be assi-
milated to Pterocerian beds elsewhere. The succeeding series
commences with a very characteristic group of rocks, part of which
forms a great bank with white veins on the shore north of Boulogne ;
and 18 feet of it is quarried along the sides of the great valley be-
tween Mont Lambert and the sea. It is everywhere fossiliferous,
the most abundant fossils being Ammonites longispinus, Trigonia
Rigauxiana, Pholadomya acuticosta,Gervilliakimmeridiensis, Exogyra
virgula, Terebratula subsella, and Serpula tetragona. This bed forms
the base of a series of great thickness, in the centre of which comes
the conspicuous mass of soft sand with large cheese-doggers (L of
M. Pellat, 33 and 34 of M. Hébert), which is only seen at La Créche.
This makes no show on Mont Lambert, and is probably quite a local
deposit. For purposes of comparison it is well to pass over these
minor distinctions, and to place all the mass K LM of M. Pellat in
: 2P 2
564 J. F, BLAKE ON THE UPPER
one division, or zone, of Amm. longispinus. The upper portion is
very shaly, and contains, on both sides of Boulogne, Lingula ovalis,
Trigoma variegata, and Thracia depressa. The upper limit of this
is assumed by M. Pellat to be the remarkable lumachelle of Hxogyra
virgula, which stands out as a broad band in the cliff of Chatillon,
but which unfortunately is absent from La Créche. The base of
the ‘‘ Portland” was originally taken by M. Pellat (39), as by all
others, below the great conglomerates ; he subsequently included all
M as “ Portlandian ” (62), but finally (68) took only the upper halt.
Certainly the beds become sandy by degrees, and, for some distance
below the conglomerates, begin to indicate coming changes, as may
be seen both at La Créche and Gris Nez. This change, being
accompanied by the introduction of a new fauna, including Ammo-
nites gigas, Cardium morinicum, Trigonia Mumeri and T. barrensis,
Perna Bouchardi, and Hemicidaris purbeckensis, may well justify
the lowering of the line of separation, as we so often have to do,
the paleontological change being accomplished more quickly than
the lithological.
The next portion of the series is perhaps the most interesting of
all; and as it is chiefly exposed along the coast, we here reap the
benefit of M. Hébert’s admirable and accurate researches, which
may be referred to for the closest details (37). He describes the
three chief localities where these rocks may be seen, viz. :—to the
south of Boulogne, from Chatillon to Kquihen; to the north, from
La Créche to Wimereux, and at Gris Nez. The shales last noticed
are the No. 26 of his sections, and from their thickness form an
admirable base. The lowest bed of the ‘“ Lower Portlandian” at
La Créche is a 3 to 4-foot band of excessively hard crystalline cale-
grit, blue in the interior and without fossils ; it is followed by grey
fucoidal doggers in sands or clays (not well seen) for 10 feet or
more; above come 4 feet of hard yellow sandstone rock, full of a
quartzose conglomerate, and a perfect lumachelle of Hxogyra virgula,
covered by a layer crowded with Trigoma Pellats and T. Mumeri,
and then passing into 4 feet more of ferruginous conglomeratic grit
with the same fossils. These are Nos. 23-25 of M. Hébert. Seeking
these on the Portel side, we find the crystalline grit attached here
and there to the base of the great conglomerate, but very irregularly;
towards the north it sinks by degrees till, opposite the Fort du Mont
Couple, it is on the sea-shore. Here it encounters a considerable
fault, running nearly parallel to the cliff, and just cutting behind the
nearest cliff-quarries of Chatillon*. It is thus thrown to the top of
the cliff, and forms the base or perhaps the greater part of the
materials worked there, being in both places crystalline and ligni-
tiferous, and overlying the shales more or less unconformably.
Above it comes a variable mass of sands and clays, with huge grit
* T at first thought the appearances were due to a local erosion and an over-
lap of the Chatillon beds; but MM. Sauvage and Rigaux suggested a fault,
the direction of which was made clear by the observations of Prof. Prestwich
during an excursion of the Geological Society of France in September 1880.
=
JURASSIC OF THE PARIS BASIN. 563
doggers, often becoming continuous, which develop to a considerable
thickness at Chatillon, are worked there and at Mont Lambert, and
constitute the base of Gris Nez. These are capped by the great
ripple-marked conglomerate, distinguished everywhere by the abun-
dance of Hwogyra virgula, Trigonia Pellati, and 7. Mumeri, which
becomes, however, a mass of false-bedded sand with hard doggers
at Gris Nez. These are so associated with the sands below, that
the natural subdivision would seem to be made above them, where
Hz. virgula ceases to be a common fossil; and these two parts,
N,, N, of M. Pellat, 23-25 of M. Hébert, may form the zone of
Ammonites gigas, which certainly occurs throughout.
The next zone is the chief fossiliferous one. It consists, at the
base, of soft marly sands with hard bands, N, of M. Pellat, charac-
terized by Perna Bouchardi ; next, of some hard grits in more than
one bed (N*), with Cyprina Brong gnarte, Plerocera oceant?, Natica
Marcousana, and Hemicidaris purbeckensis; and, finally, of earthy
beds and sands more or less ferruginous and consolidated, with
rolled pebbles and local unconformities. The whole of this does
not occupy more than 20 feet at La Créche. At Portel the middle
portion is nodular, and the whole is thicker. At the quarry of
Mt. Lambert, nearest Boulogne, the whole appears as massive sand-
stones; but at Gris Nez the most instructive section occurs. On the
east of that point the marly beds are crowded with Perna Bouchardt
and many other fossils; over these come the hard grits with Cyprina
Brongmartr, forming a well-marked feature; and above is a local
band of green earth, followed by a conglomeratic sandstone and
sand, which in the cliff on the south appear to thicken out to nearly
30 feet. The whole in the first locality is overlain by the shales of
the “Middle Portland,” not previously noticed here. The nodular
character of these upper sandstones is noted by M. Hébert in his
No. 17' of La Créche. With regard to the fossils, Trigonia Pellate
extends to the top at Gris Nez, and so does Ammonites gigas at La
Créche, according to M. Hébert; the others noted are Nerita transversa,
Orthostoma Buvigniert, Corbula autissiodorensis, Corbicella Bayan,
Mytilus Morrisu, Pecten suprajurensis, Corbula ferrugmea, from
the Perna-beds; and from the grits and sands, Twrritella Semanna,
Acteonina Davidson, Paleomya autissiodorensis?, and Ostrea rugosa
in addition.
The succeeding series, constituting the “ Middle Portlandian ” of
M. Pellat, is very well marked. It commences at the base with
some 30 feet of black, almost paper, shales, very similar to those of
Hen-cliff and of the Upper Kimmeridge of Lincolnshire. These are
followed by several cement-stone bands, two being especially con-
spicuous; and then more shales, with a lumachelle of Ostrea dubi-
ensis at the top, making a total of about 50 feet. The fossils are, as
usual, flattened in the shales, and in places are innumerable. The
most important species noticed were <Alaria cingulata, Astarte
scalaria, Cardium morimicum, Lucina minuscula, Mytilus autissrodo-
rensis, Anomia suprajurensis, Discina latissima, and Avicula octavia
566 J. F. BLAKE ON THE UPPER
in the lumachelle. These beds form the O, of M. Pellat, and
the middle of Nos. 15-17 of M. Hébert. They are seen at the top
of the cliff east of Gris Nez with the usual Astarte. Above these
the beds become softer and more glauconitic by degrees, the lowest
being a very fossiliferous band with Lima boloniensis, over which is
about 48 feet of clays, the upper half of which is more sandy and
full of hard bands, and forms a better cliff, the limit upwards being
drawn where the sandy clays cease to be glauconitic and to have a
blue tint. Lithologically these beds have a very close resemblance
to the upper portion of the Kimmeridge Clay of Chapman’s Pool,
which likewise becomes more glauconitic, and passes gradually into
Portland sands, and thence to the Flinty series. The fossils here
noted were, in addition to the Lima mentioned, Ammonites pseu-
dogigas, Belemnites Sourchii, Plewrotomaria Rozett, Myacites jurassi,
Astarte Semanni, Trigonia concentrica?, Mytilus unguiculatus, Pecten
lamellosus?, P. Morini, Perna Bouchardi, Avicula octavia, Plicatula
Boisdimi, Ostrea expansa, O. bruntrutana, Acrosalena Kengi, Cr-
daris bolomensis, and Serpula triserrata.
The highest beds of the series (P,, P,, P, of M. Pellat) are only
seen in the cliffs on either side of Wimereux to the north, and of
Portel to the south. The base consists of about 9 feet of sand and
sandstone with fucoidal markings, like the flinty beds of St. Albans;
and these contain abundance of large Cardiwm Pellati, and some
Trigonia gibbosa and other shells closely imbedded. Above is a
shell-bed crowded with Serpula gordialis, just as happens at Port-
land and St. Albans. Natica ceres and many small Cerithia are
here abundant. The succeeding rocks are more calcareous repeti-
tions of the same kind, all the hard parts being fair limestones, and
the softer quite sandy, making a total of about 15 feet. The lime-
stones are exceedingly fossiliferous, having yielded M. Pellat nearly
70 species; but the whole remains of the same character as the
Flinty Series of St. Albans, though in the latter case the sands have
been consolidated into flints. The other most noticeable fossils
appear to be Ammonites bononiensis, Natica elegans, de Lor., Ceri-
thium Manseli (near the top), C. pseudo-excavatum?, C. septempli-
catum, Pleurotomaria Rozeti, Trigonia incurva, T. Carre, Astarte
rugosa, Corbicella Pellati (?=Sowerbya Duker [cast]), Cardiwm
dissimile, Pecten lamellosus, and Echinobrissus Brodier. The over-
lying strata are of very peculiar character, bemg mostly composed
of calcareous rubble and tuff, in which there are scarcely any recog-
nizable fossils; and such as are recorded (Astarte socialis, Cypris,
Cyrena Tombecki, &c.) are not known in English Portland rocks.
The irregular manner in which these lie, aah ferruginous beds
intercalated in places, according to M. Pellat, forbid us to look upon
them as certainly equivalent to the Portland building-stones, which,
as a lithological group, or as a paleontological horizon containing
Ammonites giganteus (true), Bucconum naticoides, B. angulatwm, and
Cerithium portlandicum, are not here to be found. There is, in fact,
no proof that any thing but Wealden beds overlie the Flinty Series at
Boulogne.
JURASSIC OF THE PARIS BASIN. 567
Discussion or Resutrts.
From the above observations it is proposed to classify the rocks
under consideration as follows :—
1. PortTLANDIAN.
Upper = Purbeck.
Lower= Portland Limestone.
2. Bowontan.
Upper =“ Middle Portland.”
Lower =“ Lower” Portland.
3. KIMMERIDGIAN.
Virgulian.
Pterocerian.
Astartian.
4. CoRALLIAN.
Supracoralline.
Coral Rag.
Coralline Oolite.
. OXFORDIAN.
(2)
_ f Oxford Oolite.
Upper = | Oxford Grit.
Lower = Oxford Clay.
The first point to be considered is the upper limit of the
Oxfordian group. When the English classification is compared
with the French, serious discrepancies are found to exist; for
our Lower Calcareous Grit, and part at least of our Coralline
Oolite, are in France universally placed in the Oxfordian. In the
Ardennes department it has been seen that grits which underlie the
Neuvizy ironstone correspond both in character and contents with
the Nothe Grits and the Calcareous Grits of Yorkshire up to the
Passage-beds ; yet these are placed as Middle Oxfordian by Sauvage
and Buvignier(2). The richly fossiliferous ironstone forms the type
of the Upper Oxfordian for all French geologists; and when we trace
its range and that of the rocks which overlie it, this seems justified
stratigraphically. For above it lies a series of very changeable lime-
stones, contrasting in this respect with the uniformity of the iron-
stone ; and these same limestones, after the ironstone has died out,
are carried on in a recognizable form over other Oxfordian beds.
Thus the independence of the two groups is most marked where
the dividing line is drawn. The Paleontological separation is also
well marked ; for out of the 154 species recordedby Buvignier from
the ironstone in the Meuse, only 45 pass upwards to any member
of the Coral Rag. Excluding the Creué limestone, which forms a
kind of passage-rock, the difference is equally marked wherever the
fossils have been sufficiently studied, as in the Yonne, where Cotteau
shows (16) that, out of 323 species in the lowest Corallian beds, only
17 occur in the Oxfordian, if we draw the line between the two
groups as proposed; and even where the lithology is the same,
568 J. F. BLAKE ON THE UPPER
only 17 out of 58 are common. If, then, by stratigraphy, by
paleontology, and by common consent, the Neuyizy ironstone
and its equivalents are to be placed as the summit of the
Oxfordian, the English classification must be modified to bring it
into harmony with more widely-established facts. It has been seen,
in former studies of our English Corallian rocks, how readily they
lend themselves to such a change by the ‘“‘markedly Oxfordian
character of the fauna” of their lower part. It is proposed, there-
fore, to abolish the term ‘‘ Lower Calcareous Grit,” as associating
the rock intended too closely to the “ Upper Calcareous Grit,” and,
as it forms an integral part of the Oxfordian series, to call it the
‘‘ Oxford Grit,” and, for some part at least of the overlying lime-
stones, to revert to the old name of the “‘ Oxford Oolite.” These
terms, however, are too descriptive to be generally applicable, and,
when they are not so, may be replaced by the more general term
‘¢* Upper Oxfordian.”’
We may now trace the range of this mass over the area
studied. ‘The Ferruginous Oolite of Neuvizy has been placed as
the Lower Oxfordian by Oppel (27), partly in reliance on Prof.
Hébert’s erroneous section (21), which places a mass of clay
above it, partly by placing the Crdaris-florigemma beds as Upper
Oxfordian, but chiefly by including the whole of the underlying clay
in the same subdivision, and thus quoting true Oxford-Clay fossils,
which are not to be found in Buvignier’s lists, such as Amm. biarmatus
and Amm. Henrici. Oppel does not, however, quote Amm. Lamberti,
which is most characteristic of Oxford Clay. There is not sufficient
evidence, therefore, to overcome the weight of that obtained from
the list of fossils given above, which places this ironstone as the
uppermost part of the Oxfordian, as it is stratigraphically by its
immediately underlying the Cidaris-florigemma beds. Along the
whole of the Eastern range, the Oxford Grit below remains constant,
becoming more nodular to the south; and the ironstone reaches
nearly as far. The only ‘deposit hereabouts which can give rise to
any dispute is the limestone: of: Creué and Liouville, the highly
Oxfordian character of the fossils in which has led Hébert (21) to
place it in the Oxfordian ; while Buvignier (22) makes it Corallian.
Paleontologically, itis undoubtedly more united to the Oolite below ;
but by its extremely local character, and its alternating with the
Rag above, it belongs more to the latter, and must therefore be left
as on a kind of neutral ground.
On the change of strike and on crossing the band of Lower Jurassic
rocks which extends to the south, we find a change in the development.
Grits and ironstones can no longer be found, but the rocks continue
to be marly as below; while a new set of Ammonites characterizes
the upper part, though the general facies remains the same, the true
Oxford Clay, with Lon. Babeanus and Amm. Lamberti and others
belonging to the group Harpoceras remaining constant. Below, it
would appear that the beds which ‘intervene between these and the
Corallian, with their Ammonites continuing from below, as Amm.
marantianus &c., occupy the place of the Oxford Oolite and Oxford Grit,
JURASSIC OF THE PARIS BASIN. 569
and are therefore the Upper Oxfordian. Tombeck (50, 55,57, 64, 65,
66) endeavours to show that the zone of the last-named Ammonite
is above the Coral Rag ; but, his stratigraphy not being accepted, no
proof or probability exists of its occupying so anomalous a position.
Three are certainly great differences of opinion on the true position
of the zone of Amm. tenwilobatus, which in the Jura is supposed to re-
present this—some, as De Loriol, Mésch, Bayan, &c., considering it
Astartian, and others, as Hébert, Dieulafait, &c., making it Ox-
fordian. It would be hazardous to venture an opinion on this point
before studying the localities; but the fossils have an Oxfordian
facies; and if the zone really corresponds to that of dmm. marantianus
in the Haute-Marne, it is certainly not Astartian. These are the so-
called Marls without fossils, both Upper and Lower, which have never
been seen separated by any true Diceras-beds. They form the base
at Les Laviéres, Vouécourt, and Buxiéres ; and the lower part of the
same mass constitutes the marly limestones of Maranville, and the
upper the cement-stones of Clairvaux, in the Aube. Further west,
in the valley of Laignes, the gritty character comes in again, with
similar fossils to those in the Meuse. In the Yonne we find the
true Oxfordian marls with their Harpocerata at Ancy-le-Franc, and
above these the Upper Oxfordian, in the new form of massive cal-
careous sandstone, at Pacy, in the valley of the Armancon. The iron-
stone of Ktivey has unfortunately not been examined ; but by its
fossils it might well represent the Oolite of Neuvizy, except for
Ammonites lunula. In the neighbouring valley of the Yonne the
Upper Oxfordian is recognized in the siliceous limestones underlying
the great white limestones of Coulanges, referred to the Corallian.
Great differences of opinion have been expressed about the correlation
of this portion. In their general work Leymerie and Raulin (25)
placed the Ktivey ironstone as Lower Oxfordian, as also the beds at
Ancy-le-Franc, which they nevertheless considered lower still. The
Pacy freestones they called Middle Oxfordian, and paralleled with
the Coral Rag of Chatel Censoir, leaving the lithographic limestones
only to represent the Upper Oxfordian. © This, however, has been
proved to be wrong by Cotteau (16, 34), who showed the essen-
tially Corallian character of the limestones of Coulanges and of
Vermanton, and discovered the Coral Rag at the base of the litho-
graphic limestones. The fossils and the stratigraphy are all in favour
of the latter author’s view. M. Hébert (21, 31) recognizes in
the Etivey ironstone an equivalent of the Neuvizy, and says it
plunges beneath the limestones of Ancy-le-Franc. The latter thus
becomes his Upper Oxfordian ; and in the same horizon with it he
places the freestones of Pacy, which are the equivalent of the upper
part only, and the limestones of Vermanton, which have been proved
Corallian. He considers it also the equivalent of the Creué limestone,
which is above the Ferruginous Oolite. Some of these correlations
may be rejected : but there is unanimity on the Pacy freestones repre-
senting the Upper Oxfordian, in spite of the recorded presence of
A. Babeanus. In the valley of the Loire the Upper Oxfordian is lost
in the unfossiliferous marls; and in that of the Cher it must lie in
570 J. F. BLAKE ON THE UPPER
the lithographic limestone mass, since the fossiliferous sponge-bed
is characterized by Ammonites canaliculatus and other species be-
longing to a lower horizon, though the recorded presence (60) of
A. marantianus shows that we are there not far off the top. In the
Lower Charente, the locality Marans has beds below any thing seen
at La Rochelle. In the Sarthe the description of M. Hébert (21)
would lead us to place his ‘‘ Middle Oxfordian” as Oxford Grit, which
here returns to its usual character, and his ‘“‘ Upper Oxfordian,”
which is here marly, as Oxford Oolite. On the coast of Calvados
we find in the Trouville Oolites, seen in true succession in the cliff
of Auberville, a good paleontological representative of the Neuvizy
ironstone; and below comes the Oxford Grit, with an equally cha-
racteristic fauna. The lower of these two beds is considered by
Hébert (28) to be Middle Oxfordian, and therefore to correspond to
the Neuvizy ironstone, and the rest to be Upper Oxfordian ; but the
Neuvizy ironstone is certainly more allied paleontologically to the
upper beds, and the grits associate themselves with these more
completely than with the beds below.
The series here, as has been seen, corresponds exactly with that at
Weymouth—the Nothe Grits,the NotheClays, the Bencliff Grits, and the
Osmington Oolites all following regularly. The last named, therefore,
are to be specially paralleled with the Neuvizy ironstone, with which
they have 29 per cent. of their fossils in common, and must be called
Oxford Oolite,and the grits below, Oxford Grit. Whether the Trigonia-
beds of Weymouth are to be also included is a more difficult matter,
to be discussed hereafter ; but we must certainly place on the same
horizon the pisolites of North Dorset and the oolite of Highworth,
which has 57 per cent. of its fossils common to Neuvizy, and perhaps
also the road-stones of Faringdon. Unfortunately at Oxford the ~
“Oxford” Oolite is not well represented, except near Marcham. At
Upware the limestones of the north pit belong here. The great
development in Yorkshire gives us for the Oxford Grit the whole
mass up to and including the Passage-beds, and for the Oxford
Oolite as far up as the Trigonia-beds of Pickering, the latter having
55 per cent. in common with Neuvizy. In fact, the greater part of
the limestones which underlie the Coral Rag proper belong to this
portion.
Our circle is finally completed in the Boulonnais, where the
limestone of Houllefort, in the midst of clays, offers us the only
representative of this part of the series, though to what exact part
it may be considered to correspond may be doubtful. The excep-
tional presence in it, however, of Cidaris florigemma indicates a high
position. :
We have next to discuss the Corallian series. De Loriol (50,
56) and Tombeck would have us abolish the term altogether ;
and Oppel (27) practically does so by including his “ zone of Cidaris
florigemma” in the Oxfordian. The argument against its use is that
coral-growth is only an accident which may happen at any time,
and that there is much of the so-called Corallian which has no corals
in it. These statements are doubtless true, and yet, to one who has
JURASSIC OF THE PARIS BASIN. 571
traced the series from end to end of the Paris basin, they seem to
have no weight. The Corallian series, as now to be limited, is one
of the best-marked groups it is possible to conceive; but, as Buyig-
nier (22) has so well expressed it, its constant feature is inconstancy.
Below this group we may have some continuous beds; above it the
beds are markedly continuous ; but within it discontinuity is the rule.
It is quite to miss the mark, therefore, to say, as Tombeck says
(50 &c.), that its normal form is the compact limestone, and coral-
growths and Diceras-beds abnormal. Noone kind of deposit is more
normal than another, except in this way, that the variety which is
most frequently repeated, and which occurs at several horizons and
under the most varied forms, is a coral-growth, and neither above
nor below the limits of this series can such coral-growths be found
in the country examined. Hence, unless one were to invent a new
term, such as Protean, to indicate variability, no better name could
be chosen than Corallian to indicate this most name-needing group.
In the study of the English Corallian we have stated* that the
Coral Rag, with Cidaris florigemma, is always at the top of the
limestones, while the French geologists have asserted it to be as
constantly at the bottom. This anomaly is now explained. By
marking off so much of the so-called Coralline Oolite to place it in
the Oxfordian, we leave the Coral Rag nearly, and in most places
quite, at the base. Sometimes, as near Oxford, it lies on the
Oxford Grit ; sometimes, as at Upware, on the Oxford Oolite; and
only here and there can we suppose, and that doubtfully, that any
oolite belonging to this series rather than to the Oxfordian, and
hence to be called Coralline Oolite, intervenes. It may beso at
Malton and Seamer, in Yorkshire, especially where shell-beds are
developed; and it may be so at Weymouth, where we may possibly
call the Trigonia-beds by this name. As for Cidaris florigemma, it
is characteristic of the Corallian as a whole, and is perhaps not con-
fined to it. Tombeck describes (55) a bed abounding with it at
St. Ansiau, in the Haute-Marne, supposed to lie in the Oxford Clay,
though a fault is here possible ; and the Houllefort limestone, which
cannot be called Corallian, contains it ; on the other hand, it is found
in Astartian beds at Weymouth. But, after experience of its habit,
it is impossible to say more than that it is commoner towards the
base than towards the top of the Corallian series, and is usually asso-
ciated with massive corals. As to there being a bed full of it con-
stantly marking the junction with the Oxfordian, as Hébert says
(21), this is a feature that seldom occurs.
The upper line separating the Corallian from the Kimme-
ridgian is rather hard to draw. Tombeck says (50) that, if
we take the so-called Astartian as the base of the latter series,
it cannot be drawn paleontologically; and de Loriol (50, 56),
on the strength of this, wishes to call the Astartian and Coral-
lian by one name, Sequanian. On the other hand, Hebert (19,
31) says that one can put one’s finger on the line of junction, and
* Blake & Hudleston, Quart. Journ. Geol. Soc. vol. xxx. p. 313 &e.
572 J. F. BLAKE ON THE UPPER
that the two series are perfectly separate by their fossils. The
latter supposition we may dismiss, as it is exceedingly improbable ;
and it has been shown(p.529)that in the Aube several such apparent
junction-lines occur, one above the other. On the other hand, Tom-
beck’s statements appear to be vitiated by his including the Oolite of
La Mothe in the Astartian, instead of associating it with the Diceras-
beds ; and if this rectification were made, we should find one palzon-
tological distinction indicated by himself—namely, that while the
Corallian contains the zone of Cardium corallinum, the Astartian con-
tains that of Verebratula humeralis. Admitting, however, that the
actual line may be rather arbitrary, and that some Corallian forms
occur above it, and even Oxfordian ones, 1f Ammonites marantianus
be truly recorded, yet if it be drawn not far above the Diceras-beds
and ther equivalents a change is soon perceived after the line is
‘passed, as will be shown in the sequel We shall then have three
subdivisions in the Corallian series, which may or may not be deve-
loped in any particular locality,and the distinctness of which may often
be lost, but which are nevertheless sufficiently constant to make it
important to recognize them. ‘The upper division, or “ Supracoral-
line,” almost wants a better name than it has received. Its most
remarkable form, the Diceras-beds, would almost induce us to apply
that name, but that the form is too local. The term *‘ Supracoralline”
1s applicable in the great majority of cuses ; but the beds must not be
supposed to be always above the actual coral-growths. The middle
division, or ‘Coral Rag,” is so called to denote the more common |
position of the Astraan corals, generally associated with Crdaris
florigemma, though this portion may be without such corals, which
may occur above it instead. And the lower division, or ‘ Coralline
Oolite,” represents those limestones which lie in certain places above
the best representative of the Upper Oxfordian in the district, and
yet below the beds identified as Coral Rag: it is a division which in
most districts may be ignored.
We must now trace these beds in their range. In the Ardennes
we find, immediately above the Ferruginous Oolite, a comparatively
thin bed of crystalline coralliferous limestone, with Cidaris flori-
gemma, which may be recognized at once as the Coral Rag. Itis sur-
mounted by the magnificent limestone of Novion, in which Crdaris
florigemma is rare, if present, but which contains Cardiwm corallinum
and some Dicerata. These, though full of corals, are the Supracoral-
line beds, becoming oolitic above, and affording no well-marked upper
limit. On entering the Meuse we immediately find the Coral Rag to
have increased, and to have developed various forms, such as oolites
and crinoidal limestones. There is, however, no regularity in these
minor beds, since near Verdun the crinoidal limestones are beneath
coral-growth, whereas near St. Mihiel they cap it. Near Verdun
some shell-beds are found which might be called Coralline Oolite.
The Supracoralline beds are much thicker. In fact, if we are to keep
the Astartian beds at all comparable to each other, and to include
all rocks of the Diceras-bed type in the Corallian, we must absorb
into the latter a considerable portion of Buvignier’s Astartian. At
JURASSIC OF THE PARIS BASIN. 573
St. Mihiel we have a thin bed below the coral-growth, which is best
ealled Coralline Oolite ; and it is probably the end of the great lime-
stones of Creué, which also will be placed as such. Buvignier has
himself (22) recognized that the Coral Rag of St. Mihiel is no other
than that of Verdun, and it is only one facies of the beds of this age.
The Supracoralline division retains its former character, but begins to
have true Diceras-beds on the top, especially in the south (21). In
the extreme south the Coral Rag develops into avery thick mass, which
is very rubbly and fossiliferous towards the base, with Cidaris flori-
gemma &e., surmounted by white chalky limestone, and finally by
compact limestone beneath the Astartian beds; so that here the
distinctions of the two parts of the Corallian are less marked. In
the Haute-Marne, at Reynel, in the east, the rubbly Coral Rag occu-
pies the base, and more compact limestone lies above it (55), with a
development of the Diceras-beds above. Inthe valley of the Rognon
there is a band of disaggregated Oolite at the base (19), then a fine
development of the Rag, and a magnificent display of the Supracoral-
line beds in the form of pisolites with Diceras, with compact and
oolitic beds associated, up to the more marly Astartian beds. Inthe
valley of the Marne the Supracoralline Diceras-beds have become the
summit ; and beneath come the massive coral-growths with Cidaris
florigemma, occupying a great thickness, and having below them
massive limestones, which might be called Coralline Oolite ; but as,
according to Royer(12), they have rubbly rag below them at Soncourt,
they must be placed as a development of the Coral Rag. Passing
west towards the Aube, the Diceras-beds become more restricted, and
confined to the upper part, as at La Mothe, while the coral-growth
or rubbly beds beneath lose their character, or remain as shelly lime-
stones only. On reaching the valley of the Aube itself, all is united
in an undistinguishable mass of limestone, with only a shelly repre-
sentative of the Supracoralline beds; and Astartian and Corallian
form one massive, lying on Oxfordian marls at Clairvaux, and
covered by Pterocerian marls near Bar-sur-Aube. ‘Travelling west
to the valley of the Laignes, new developments arise. The thin shelly
band is replaced once more by Diceras-beds of considerable thickness,
and the beds below put on a characteristic form at the base; for
below a mass of compact and false-bedded limestone comes a rubbly
mass of coral-growth, full of the shells which usually accompany it,
though Cidaris florigemma was not noticed. This again might be
called Coralline Oolite, but that it is believed to develop into Coral
Rag later on. In the valley of the Armancon this lower shelly mass
has again dwindled down to a narrow band; so that it was left to
Cotteau, or rather to M. Lettéron (438), to discover it, filled with corals
and the usual shells and echinoderms, underlying the lithographic —
limestones. This discovery seems to give the coup de grace to the
idea of the latter being Upper Oxfordian (25). They are, in fact,
the continuation of the compact limestones of the Laignes valley ; and
in various beds contain a Corallian fauna, the uppermost of which,
met with by M."Hébert near Angy, seems to have led him (31)to place
the limit of the Oxfordian too high, 7. ¢. above instead of below the
574 J. F. BLAKE ON THE UPPER
lithographic limestones, which are very different from the limestones
of Pacy. In fact, the limestones of Angy and Tonnerre are shown
to be the Supracoralline beds, and do themselves contain Diceras-beds,
especially at the top, though the whole is enormously developed, so as
easily to mislead one. On passing westwards, however, to the valley
of the Yonne, still more is in store ; for while in the neighbourhood
of Bailly and Vincelles the Supracoralline beds occur in all their
characters, beneath them are still found the lithographic limestones,
more than usually marly at Vermanton; and below these again the
coral-beds of the Laignes valley, so much reduced in the Armancon,
burst out into a magnificent mass, wherein corals of all kinds,
Diceras, Nerinewa, and all the Rag fauna are confusedly mixed in ex-
treme abundance, as may be seen so well at Merry-sur-Yonne,
Chatel-Ceusoir, and, in a more uniform character, in the white lime-
stones of Coulanges. It is this development that for ever negatives
the idea that Diceras-beds are necessarily above the Coral Rag, though
these Dicerata differ from those of the Diceras-beds in apparently
having lived near the spot, and in not having been rolled. Beyond this
valley the Corallian once more changes, and by degrees returns to the
dead uniformity of a lithographic limestone. In the valley of the
Loire the lower Diceras-bed is seen in diminished thickness near La
Charité, succeeded in an upward direction by compact limestones,
which show no more character than that of becoming oolitic near
Pouilly. On the left bank of the river, however, it is stated (32, 60)
that the Lower or Coral-Rag Diceras-beds are not to be found, but that
the Supracoralline ones are once more developed at Sancerre. These
last take up again their Armancon form near Bourges, and show, not
quite at the summit, the white limestones of Angy and Tonnerre.
Hence to the Cher is the path of degradation ; for in the latter valley
even less can be distinguished than in that of the Aube, but all is
lithographic. In the Charente department the Corallian rocks remain
still massive and but slightly characterized, though coral-beds are
developed in what may be considered the equivalent of the Coral Rag.
The Supracoralline beds are still characterized by the abundance of
Nerinee and by the presence of Diceras and Cardium corallinum.
In the Lower Charente, on the shores of the Pertuis d’Antioch, the
Corallian rocks put on a fresh form, the lower part being a white fos-
siliferous limestone, which, by its fossils, may represent the Rag ;
while the true coral-bearing beds are on a horizon usually “ supra-
coralline,” and are parallel with the similar development in the
Ardennes. It would appear that d’Orbigny included still higher beds
in his ‘ Etage Corallien’ here ; but a comparison of the series in the
two Charentes and the general fauna indicate the necessity of draw-
ing the line separating the Corallian from the Astartian almost
immediately above the coral-reef of the Point du Che. In the
departments of the Orne and Sarthe, according to Hébert’s descrip-
tion, there would appear to be no development of corals on the usual
horizon ; but the Supracoralline beds contain Diceras and are over-
lain by coral-growth, which is thus on a higher horizon than almost
anywhere else.
JURASSIC OF THE PARIS BASIN. 575
On the coast of Calvados the sequence is tolerably plain; for
the beds characterized by Cidaris florigemma succeed immedi-
ately to the Trouville Oolite, and thus occupy the base. They
change laterally into coral-growth, which represents the Coral
Rag; so that there is little, if any thing, that can be called * Coral-
line Oolite,” unless it be the mass that underlies the Rag in the
Trouville quarry. The Supracoralline beds are here quite different
in form from those in the southern range, being arenaceous, instead
of calcareous or coralliferous ; nevertheless they contain calcareous
matter, and are admirably marked off stratigraphically from the
beds above by the difference of lithological character. The arena-
ceous character of these beds appears to prevent their assimilation
palezontologically with their calcareous representatives, the two sets
having little in common; nevertheless the fossils afford no nega-
tive to their stratigraphical correlation. In the well-known neigh-
bourhood of Glos, in like manner, can be traced the Coral Rag in
all its commonest characters, with perhaps a representative of a
Coralline Oolite below. Above, we appear to have a twofold de-
velopment of Supracoralline beds :—one, at the base, being calcareous
and similar to the Novion limestone and other southern supra-
coralline beds, wanting only the Diceras, but with abundance of
ramose corals; the other, above, being an enormous development of
loose sand, corresponding to similar beds on the coast, and containing
a fauna which indicates a high position. These sands were placed
by Zittel and Gouert (under the guidance of Hébert) as Upper
Corallian, which corresponds to the above-assigned place. Their
relation to the coast-beds, and the correspondence of the latter to the
Sandsfoot-Castle beds of Weymouth, leave no doubt that the latter
must, with them, be placed as Supracoralline. We come thus to the
discussion of the Corallian of Dorset. There seems little doubt that,
the Sandsfoot-Castle beds being Supracoralline, and the Osmington
Oolite Upper Oxfordian, we must find the beds corresponding to the
Coral Rag between these limits. What actually does intervene is
the Sandsfoot Clay and the Trigonia-beds. The abundant fossils of
the latter still leave some doubt as to its proper position. On the
one hand, such fossils as Gervillia aviculoides, Ammonites cordatus,
Pecten fibrosus, and Echinobrissus scutatus are extremely Oxfordian ;
while the presence of Ostrea deltoidea, Cidaris florigemma, and
Thamnastrea arachnoides attaches the rock to the Corallian. The
knot can only be cut by calling it a passage-bed, or by placing it
with other similar puzzles as ‘‘ Coralline Oolite.” It cannot, how-
ever, properly represent the true Coral Rag ; and thus we are driven
to look upon the Sandsfoot Clay as being its equivalent here, a cor-
relation not without value when other northern localities are con-
sidered. In North Dorset the lower limit of the Corallian, as now
defined, is very well marked; for the uppermost Oxfordian is the
false-bedded series, and the overlying rubbly beds with Cidaris flori-
gemma cut off the upper edges. Nevertheless the paleontology is not
altogether satisfactory ; and we are obliged to allow a wider range
than usual for more than one characteristic fossil, ¢. g. Echinobrissus
576 J. F. BLAKE ON THE UPPER
scutatus and Hemicidaris intermedia. At Westbury the Corallian
would appear to be almost absent ; for we must now refer the rubbly
beds with Hehinobrissus scutatus to the Upper Oxfordian, and the iron-
ore itself is nearly, if not quite, Astartian. The ferruginous cha-
racter of rocks appears in some way connected with such gaps. In
the neighbourhood of Westbrook, Wiltshire, a coral-bed has been
described* from which Cidars florigemma is absent, and which,
on that account, is considered older than the usual Rag. This may
be so; but, in view of the similar Rag in the Aube department
passing into a true florigemma-lKag in the Yonne, the difference can-
not be of much importance, either here or elsewhere. It certainly
need not be considered an Oxfordian reef. Atthe Calne quarries the
lower clays, like those of Hillmarton, abound in Crdaris florigemma,
and the bed with Hemicidaris intermedia occurs towards the base ;
hence an examination of these quarries alone might lead a foreign
geologist to call the freestones Supracoralline ; but the error of such
a correlation is easily proved by the overlying coral-growths observed
in the heights on the north and south immediately beneath the Kim-
meridge Clay. There is little, in fact, in this district to represent any
Supracoralline beds. The same is true all the way to Oxford,
the ferruginous earth being the only deposit referable to them.
The only Corallian rock is the Coral Rag itself, unless we call the
great quarries at Wheatley Supracoralline, for which their great
resemblance to the limestones of the Ardennes and the Meuse
might be an argument. The arrangement of the Yorkshire beds is
not very easy, because it is rather difficult to decide which of the
beds underlying the Rag should be placed with the Oxford oolite,
and which should be associated more closely with the overlying
mass. Referring to our comparative sections (Q.J.G.8. vol. xxxiii.
pl. 12), the abundance of Hchinobrissus scutatus in the Lower Oolites
of Grimston mark them as Oxfordian; while the ‘“ mamillated-ur-
chin series,” by its Cidaris florigemma, is as plainly Corallian.
The Chemnitzia-lmestone of Malton is just one of those doubtful
deposits to which it is best to apply the name Coralline Oolite. At
Pickering the rubbly nature of the base of the Upper Limestones,
g, and the introduction there of corais, added to the change of
fauna, indicate that the base-line of the Corallian should be drawn
almost directly above the Trigonia-beds. It will then be seen that
the shell-beds at the top of the Lower Limestones are more con-
nected with the uppermost Oxfordian than with the Corallian. As
to the Supracoralline beds, they are simply equivalent to the ‘‘ Upper
Calcareous grit,” which latter is parallel to the Sandsfoot grit, and
not altogether above it as we previously supposed (Jl. ¢. p. 390),
owing to the non-recognition of the Sandsfoot clay as the equiva-
lent of the Coral Rag.
In the Boulonnais the clays with marly limestones of the Mont
des Boucards were first called Oxfordian by Rigaux (83), appa-
rently because they seem continuous with the marls below; but on
the discovery of the coral-bearing beds at the base or lower part
* Quart. Journ. Geol. Soe. vol. xxxiii, p. 288.
ld
JURASSIC OF THE PARIS BASIN. aT
(41), Pellat was compelled to place them at least as Corallian, as he
identified the Coral Rag with that of Brucdale, and, at the same time,
noted that the overlying marls are on the horizon of the compact
limestone of Vouécourt and of Tonnerre, both of which are Supra-
coralline. At a later date (56), owing to the supposed proof by
Sauvage (51) and Rigaux (53), that the equivalents of the marls of
the Mont des Boucards underlay, in the soundings, the Brucdale Coral
Rag, he met them halfway, and placed the two as equivalent. With
the breakdown of that proof is lost the necessity of disturbing the
former more correct reading, by which the coral-bearing beds of
Brucdale and the Mont des Boucards are the true Coral Rag, and the
marls of the latter place are Supracoralline, though not developed
at Brucdale. The occurrence, however, of Trigonia Bronnw in a
ferruginous bed above is too close a resemblance to the development
at Glos and Sandsfoot to allow us to place them in the Astartian ;
and we must raise the limit of the Supracoralline to, at least, the
top of this bed.
The next division is the Kimmeridgian. Its limitation above
will be discussed later on; as to its lower limit, a point much dis-
puted is, whether the beds called Astartian are to be included with
it, or with the lower beds. It is to this portion of the series, it
appears, that the term Sequanian was first applied by Marcou*; and
it was considered part of the Kimmeridgian, while Thirriay had
previously called it Astartian. Neither of the original localities for
these names has, as yet, been examined; but the latter is adopted
as most generally in use for a distinct portion of the series. De
Loriol (61) is probably the chief advocate for uniting the Astartian
with the Corallian under the term Sequanian, led thereto, perhaps,
by the supposed sequence in the Haute-Marne, and by his objection
to the term Corallian. Itis, however, noteworthy that almost every
stratigraphist separates the Astartian from the Corallian, to associate
it with the Virgulian or Pterocerian in one great group. It issoin
the description of the Ardennes(2), of the Meuse (13), and in Royer’s
original description of the Haute-Marne (4). It is not so in Ley-
merie’s description of the Aube (7), probably because he held all the
limestones at Clairvaux to be Astartian, nor in the same author’s
description of the Yonne (25). But it is practically so in Cotteau’s
description of the same (42), as the white limestone is made the
uppermost bed of his “ Sequanian,” which thus really is Supra-
coralline, and the true Astartian beds are left for the Kimmeridgian.
It is soin the Nievre (32), in the Cher (60), and in the Charente
(24); while in the Lower Charente, the coral-limestone being the
highest Corallian bed, it may be taken that the Astartian is not
specially recognized. On the coast of Normandy no one thinks of
associating the Trigonia-beds with the Coral Rag, or Supracoralline,
though they succeed the latter immediately ; and a study of the rocks
in the Boulogne area leads Pellat to the same conclusion (41).
* Recherches géologiques sur le Jura salinois, p. 116: 1846.
+ “ Notice sur le terrain Jurassique,’” Mém. Soe. 8. N. Strasbourg, 1830, p. 26.
Q.J.G.8. No. 148. 2a
578 J. F. BLAKE ON THE UPPER
There may be some difficulty in drawing a line; but throughout the
whole of the eastern and southern range one finds a marly charac-
ter of deposit setting in again over the true Supracoralline beds,
often showing much rubble and indications of local unconformity,
as we should expect on the introduction of a new series. ‘The
same is more remarkably true in the North and in England; only
in the Boulonnais is there somewhat more difficulty in drawing
the line. The fossils are usually sufficiently distinct, Terebratula
Leymervi being a characteristic form. The conclusion, therefore, so
tenaciously held by Hébert (21), seems to be the true one, that these
beds are a part of the Kimmeridgian. The thickness of the beds
assigned to the Astartian by the describers of the different areas is
very varying. ‘Thus, in the Ardennes they are said to be 21 feet,
but in the Meuse 400 feet; on the Haute-Marne, again, they are
supposed to be thin. It is plain, therefore, that a large portion of
the 400 feet (if truly determined) must really belong to the Supra-
coralline, as supposed for other reasons. ‘Their assigned thickness
in the Aube is due to a mistake, as before noted; in the Yonne
again they are called 33 feet ; in the Cher, down to the base of the
Nerinxan Oolite is 35 feet, though 80 feet more are included by
Douvillé. -The whole is therefore of comparatively small thick-
ness, and forms only a subordinate portion. The Kimmeridgian is
thus divisible into three—<Astartian, Pterocerian, and Virgulian.
The first of these is practically defined above. The Pterocerian is
adopted solely in deference to its probable justification im the area
where it was first introduced, namely the Jura, and to its distinct-
ness paleontologically when the fossils of any locality have been
carefully studied. Neither in the basin of Paris, nor in any other
part yet studied, is it sufficiently distinct to be of much importance
in the field. The Virgulian is the most easily recognized Kimme-
ridgian deposit, because the characteristic oyster occurs constantly in
lumachelles ; but itis not confined to this part of the series, either in
an upward or downward direction.
In the Meuse department, and probably in the Ardennes, the
Kimmeridgian is highly calcareous, the Virgulian portion alone
being marly. In the former there still remains some doubt as to
the true limits of the beds, and even as to their stratigraphy. While
the lower portion of the Astartian requires to be added to the Coral-
lian, the upper group appears to represent the Pterocerian as well,
from the abundance, as recorded, of Pteroceras ocean, &ce. The
lower portion abounds in the characteristic Ostrea deltowdea. As
Tombeck points out (40), the Virgulian must be made to include the
marly beds at the base of Buvignier’s “ Calcaire du Barrois,” since
these contain Pholadomya acuticosta as well as abundance of
Exogyra virgula. In the south of the Meuse department, if we
place the compact limestones in the Corallian, we find the Astartian
well characterized as rubbly limestones; and a comparison of this
locality with the Haute-Marne in the valley of the Rognon, would
lead us to commence the Astartian above the lithographic limestones
which overlie the Saucourt oolite. Nevertheless it is to be noted that
land
JURASSIC OF THE PARIS BASIN. O79
both Buvignier in the Meuse, and Royer originally in the Haute-
Marne, included the lithographic limestones in the Astartian,
and 'fombeck and Pellat do the same. It is therefore possible
that the line of junction ought to be carried further down. In the
south of the Meuse the Virgulian beds are well developed and very
fossiliferous; but the lower portion has not yet been satisfactorily
marked off as Pterocerian, although from the recorded occurrence of
Pteroceras oceant at Mauvage, and the distinct grouping of the fossils
on the several horizons, such a subdivision might doubtless be made.
Tombeck has divided his Kimmeridgian into two zones, those of Amm.
orthocera and of Amm. caletanus, corresponding to the Pterocerian
and Virgulian respectively ; and these subdivisions are accepted by
Pellat. In the Aube, contrary to the description of Leymerie, the
Astartian commences above the chalky limestone, and is characte-
rized throughout by rubbly and oolitic beds, with abundance of Tere-
bratula Leymerw. Near Bar-sur-Aube something of a Pterocerian
group may be made out; but the fossils have not been sufficiently
studied to draw a satisfactory line, which must be a paleontclogical
one. In the valley of the Armancon we have the same difficulty
as in the Yonne to decide how far above the Diceras-beds the Astar-
tian must commence, the rubbly beds next above containing rolled
corals as well as Terebratula Leymerui; but perhaps the line is best
drawn above the solid oolite block, as is done by Hébert (21) in
the neighbouring valley of the Yonne. No subdivisions correspond-
ing to the Pterocerian and Virgulian have been made out in these
western districts. Pholadomya acuticosta is the most characteristic
fossil. As to the neighbourhood of Bourges, the chief feature is the
strong development of a Nerinean oolite. The beds below this still
containing a species of Diceras, seem certainly more referable to the
Supracoralline, in spite of their lying so far above the white lime-
stones certainly recognized as the latter ; and it might be a question
whether the Nerinzan oolite ought not also to be placed below
the line of separation; but the presence of Pholadomya Protez,
Terebratula Leymern, and Trigonia Baylit may be allowed to decide
it in favour of the consensus of opinion. In the Charente, the three
portions of the Kimmeridgian are recognizable, the Astartian com-
mencing where the beds become more marly and contain Ceromya
excentrica abundantly. This latter, however, is not a fossil which
can exclude beds from being Supracoralline; and we may still re-
gard the line, therefore, as rather arbitrary. The upper two zones
are well distinguished paleontologically. ‘The same may be said of
the Lower Charente: the Astartian may be commenced with the
marly beds of the Point d’Angoulins, with abundance of Terebra-
tula Leymerii, also Pholadomya Prote: and Ceromya eacentrica, the
latter certainly becoming locally characteristic ; and the Pterocerian
and Virgulian are well distinguished, according to Hébert (54), at the
Point de Chatellailon. In Normandy, as at Weymouth, the Astar-
tian beds are better characterized than elsewhere. The change
from the calcareous grits of the Supracoralline is very marked ; and
the beds included in the zone, viz. theVillerville beds and the Trigo-
202
580 J. F. BLAKE ON THE UPPER
nia-grits of Havre, with any Ostrea-deltoidea beds above them, have
well-marked features of their own.
There cannot be any doubt of the correspondence of these beds to
those called Astartian throughout the whole of the southern range ;
and from this it follows that the Kimmeridge passage-beds of Wey-
mouth are the exact representatives of the same portion. It seems
also most satisfactory to place the Abbotsbury and Westbury iron-
stones in the same horizon, as they are apparently higher than
Supracoralline. The lowest beds of the Kimmeridge Clay seen in
the Wootton-Bassett cutting, with Rhynchonella inconstans, and the
great Ostrea-deltoidea beds of Lincolnshire, belong here also.
On the south bank of the Seine, it is prebable that at Honfleur
Pterocerian beds may be developed, though not well seen; but the
ereat mass of the clay at the Cap du Héve belongs to this division—
that is, the ‘* Marnes & Ptérocéres ” of Dollfus, and the beds nos. 7
to 14 of Lennier. In spite of the abundance of Hxogyra virgula,
and even of Terebratula Leymerw in certain beds, this portion is
well marked paleontologically by its numerous Pterocerata. The
Ammonite-marls above, so far as seen, belong to the Virgulian.
Doubtless the same subdivision might, with care, be made at Wey-
mouth ; but as yet, in spite of the many collectors who formerly
searched the shore, no Pterocerian fauna has been brought to
light. The Kimmeridge Clay of England has been shown to
be divisible into two groups*, formerly called Upper and Lower
Kimmeridge. The term Kimmeridgian must now be confined to
the latter; and though the subdivision into Pterocerian and Vir-
gulian is not very clear, it may, perhaps, fairly be taken that the
absence of Hwogyra virgula (as in Lincolnshire), indicates the former,
while its abundance (as at Ely, Swindon, and in parts of the south-
ern coast section) indicates the latter. The idea expressed in the
paper quoted, that the Lower Kimmeridge Clay represented the
Astartian, was founded on the abundance of an Astarte which at
least is very like A. supracorallina. It may, however, be distinct ;
and in any case its presence cannot be allowed to interfere with
stratigraphical conclusions supported by the general paleeontological
facies.
In the Boulogne area we have the same difficulty in drawing the
lower limit as at Bourges. While, on the one hand, there need be
no hesitation in including the Grés de Wirvigne in the Astartian,
or the Mont-des-Boucards marls in the Supracoralline, the three
intervening deposits are doubtfully attached either to one or the
other. It is certain that, in the Meuse, Buvignier would include
such beds as the Ostrea-deltoidea clays in the Astartian; yet the
ferruginous bed above with Trigoma Bronnw seems to unite both,
through the Normandy sections, to the Supracoralline, as has been
seen above, p. 563. The important MNerinwa-oolite, again, is con-
nected with the lower series by the abundance of that genus, nowhere
characteristic of Astartian, but constantly found in Supracoralline
* Quart. Journ. Geol. Soc. vol. xxxi. p. 197.
JURASSIC OF THE PARIS BASIN. 581
beds; and its complete fauna, as given by de Loriol, shows that
17 species are common to lower beds and only 10 to higher. Much
therefore might be said for making this Supracoralline ; but as there
is not much certainty about it, and it has hitherto been placed in the
Astartian, it may be left there, with the similar rock at Bourges, for
the present. Perhaps it would be preferable to draw the line im-
mediately above this, and include the F, F, of Pellat with the Gres
de Wirvigne. The fossils of the latter approximate closely to the
Astartian at Havre. The remainder of the Kimmeridgian is well
characterized here ; the lower portion, being apparently barren of
Pieroceras, would be better named after its Ammonite; but the
upper part is markedly Virgulian, and corresponds to the mass of
the ‘‘ Lower” Kimmeridge Clay (so-called) of Dorset. In the Pays-
de-Bray only this portion is seen.
For the series of deposits which overlie the true Kimmeridgian or
Virgulian, and underlie the true Portland beds, the name of Botonran
is proposed. It has already been proved* that in the Boulogne
area these rocks correspond to what had been hitherto considered
an integral portion of the Kimmeridge Clay; and Waagen (35), by
separating them as a zone above the Virgulian, came to practically
the same conclusion. For the lower portion of them, therefore, which
especially differs in lithological character from Kimmeridge Clay, and
is of the nature of an episode in its midst, the name of “ Bolognian
episode ” was formerly proposed. A further study of the same series
in the basin of Paris shows that elsewhere they are not specially epi-
sodal in character, but nevertheless require separation from the Virgu-
lian. The name Portlandian has usually been applied to them; but
since it is certain that they do not correspond to our Portland rocks,
but to beds below them, this name is to the last degree mislead-
ingy; and the only way out of the confusion is the use of a distinet
name. Seemann is said by Pellat (39) to have proposed the name
Pontidian; but as this is rejected by the latter, who alone mentions
it, it cannot be said to have priority ; and it is not a good geogra-
phical name. It seems therefore best to modify the name already
applied, and extend it to all the continental beds which, not being so,
have been called Portlandian. Some name connected with the term
“ Calcaire du Barrois” would have been better, if some true Port-
land stone had not been included in that term.
These Bolonian beds admit of a twofold subdivision in almost every
locality, though the apparently natural limits in the several places may
not quite coincide. In the Boulogne area the two parts here distin-
guished have been called ‘“‘Lowerand Middle Portland.” According
to Pellat, the fauna of the Lower Bolonian commences in the clays —
below the great conglomerates; hence the change of fauna was not
brought about by the changes of physical character, but had already
commenced. The paleontological line will therefore not coincide with
the lithological one; but the upper parts of the clay series are inde-
* Quart. Journ. Geol. Soc. vol. xxxvi. p. 189.
T Some Swiss geologists have been led by this misnomer to declare that there
are no Portland beds (in ¢heir sense) in the Isle of Portland!
582 J. F. BLAKE ON THE UPPER
pendently marked off by a change of fauna, and the “ Lower Port-
land” comes in in the midst as a true episode. This episode is less
marked in the Pays de Bray, and scarcely recognizable in the coast
of Kimmeridge, where we find the northern argillaceous type of
the Bolonian, equally marked off from the Virgulian by its fossils.
During the same epoch the southern or calcareous type was
being developed. The distinctions made in this, of lithographic
limestones, carious limestones, and tubular limestones, are too local
to be of great importance ; but the two zones of Ammonites gigas and
elther of Pinna suprajurensis or Cyprina Brongniarti are of wider
interest. These represent the bulk of the Bolonian in the southern
range. It would appear that at Boulogne the argillaceous and cal-
careous types overlapped for a while, and the paleontological divisions
scarcely coincide with the lithological. Hence if we divide the Bolo-
nian into the two parts which have the widest significance, the Lower
Bolonian, or zone of Amm. gigas, will commence with M, and end above
N, of M. Pellat (that is below the Perna-beds) ; and the Upper Bolo-
nian (or zone of Cyprina Brongmarti in the south) will include N,
and N,—that is, the remainder of the episode, together with argil-
laceous beds called ‘“‘Middle Portland.” M. Pellat includes N, also in
the upper zone; but asit contains Amm. gigas the reason of this is not
evident. The northern type may also be divided paleontologically,
independently of the forms which may be supposed introduced from
the south. ‘The lower portion appears to be characterized by Amm.
suprajwrensis (formerly quoted as “A. Thurmanni?”), and the upper
by several species, amongst which it is difficult to choose the most
characteristic. Belemnites Sowichii, Astarte Semanni, and Discina
latissima are the chief species almost confined to this portion. These
divisions would coincide very nearly with those of the southern range ;
and if with the zone of Cyprina Brongnarti were included the un-
fossiliferous grey-green limestones of the Meuse and Haute-Marne,
the periods might be considered synchronous. ‘This is very nearly
the correlation made by Pellat (59, 68); that is, he recognized in the
two fossiliferous zones his ‘‘ Lower Portland,” and in the barren zone
the possible equivalents of his ‘‘ Middle Portland.” His greatest line
of division, however, is at a different place, namely above N,. This
arrangement may be most suitable for Boulogne; but it makes the
Upper Bolonian almost absent from the southern ranges, whereas it
probably continued there in its varied forms long after the intro-
duction of clay and clay-loving forms into the Boulonnais.
Tracing these beds through the areas of their occurrence,
we find only the lower Bolonian or lithographic limestones in
the Ardennes and Northern Meuse; and from these the lower
portion of the rocks assigned to the same series by Buvignier
must be detached, as containing a more Virgulian fauna, especially .
Pholadomya acuticostata. ‘The presence of Hwogyra virgula itself
even in lumachelles cannot be made of any great importance, since
at Boulogne, throughout the southern range, and even in England
that oyster certainly survived the introduction of a very distinct
fauna of far more interest than itself. There isno sign of thinning
JURASSIC OF THE PARIS BASIN. . 583
of the Bolonian beds in the Meuse, as Hébert supposed (21); for, as
Buvignier (22) points out, the smaller quantity there visible 1s com-
posed of the lowest beds only, and not of diminished representatives
of all. On entering the Haute-Marne much more is seen, in fact
the full development, which, however, commenced near Bar-le-Due
in the extreme limit of the Meuse. The Lower Bolonian will here be
the ‘¢ Lithographic limestones” of Buvignier and the zone of Ammo-
mites gigas of Royer and Tombeck, of which, after them, the Bure
oolite may be taken as the upper limit*. The Upper Bolonian in-
cludes the more fossiliferous beds, distinguished as carious, spotted,
and tubulous limestones, and also the lower portion of the series.
called the zone of Cyrena rugosa, namely the porous limestones,
which are mostly unfossiliferous, but in places appear to contain
Natica Marcousana, avery characteristic Bolonian fossil. Passing
westwards, the tubulous limestones and higher beds are rapidly lost,
and the series is reduced in the valley of the Aube to the Lower
Bolonian and the carious limestones. These two are of longer con-
tinuance, and are found as fully developed and still more fossiliferous
in the valley of the Yonne, while they have representatives as far as
Bourges. In the Charente the sandy limestones near Angouléme give
us fair representatives of the Lower Bolonian, though with a somewhat
uncommon fauna, somewhat allying it to the Upper. This latter must
be recognized in the wide-spread limestones with Cyprina Brongni-
arte and other usual fossils of this horizon. Possibly representatives
of the Lower Bolonian exist in the Ile d’Oléron, in the limestones at
the base with A. Giravesianus ; but the great mass seen to the south
of the harbour of S. Denis is undeniably Upper Bolonian, with the
same paleontological characters as in the Charente. Neither in the
Orne and Sarthe departments nor in Normandy are beds so high in
the series reached. In the Pays de Bray the lowest Upper Jurassic
rocks are the Virgulian marls; and above them the Bolonian beds
are well developed. These are considered by M. de Lapparent (69) to
commence with his “‘beds with Ostrea catalaunica ;” while his ‘‘upper
clays and lumachelles ” and ‘‘ compact lithographic lmestones ” are
referred tothe Virgulian. Ithas, however, been shown that the top
- of the “ lower clays and lumachelles ” is exceedingly similar in cha-
racter to the base of the Lower Bolonian at Boulogne, that in the
north these contain the characteristic Tragonia Munceri, and in the
centre the lithographic limestones contain Amm. gigas, while in the
south, according to MM. Semann and Graves (39, 8), at Hodenc, a
locality coloured Portlandian by M. de Lapparent, the upper marls
(whieh are very thin in the north) contain Amm. gigas and Amm.
Gravesianus, and are followed immediately by beds with Cyprina
Brongmart. Hence it is more consonant with other localities to
commence the Lower Bolonian towards the top of the “lower clays
and lumachelles,” and end it at the top of the ‘‘ beds with Ostrea
catalawmca.” The Upper Bolonian, as before noted, commences
with the “calcareous grit with Anomias” and continues to the top
* Perhaps the beds at Cirly recorded by Tombeck to contain Amm. gigas
and A. swprajwrensis, ought to be also included in the Lower Bolonian.
584 J. F. BLAKE ON THE UPPER
of the blue marls called “ Middle Portland.” The latter undoubtedly
correspond to the beds called by the same name at Boulogne; and
the grits below represent the upper part of the so-called “ Lower
Portland,” as has been shown by Pellat (46).
In our own country the Bolonian strata are pretty nearly synony-
mous with those shown to be separable under the title Upper
Kimmeridge. Only in the coast-section of Dorsetshire has any dis-
tinction into Upper and Lower Bolonian been possible as yet; but
when once it is recognized that the whole is argillaceous, the two
parts may be some day recognized by their fossils. Throughout the
basin of Paris, however, and in the Dorset section, the lower beds are
less fossiliferous, and therefore in England they will be less likely
to attract attention in inland sections. In separating the Bolonian
from the Kimmeridge below and the Portland above, there arises in
England, as at Boulogne, the question as to their limits. In the
latter place, the ‘‘ Lower Portland ” is taken by Pellat (68) to com-
mence in the midst of marls, on account of the change of fauna.
And this change is a remarkable one; for it consists in the intro-
duction of species which do not specially characterize the episodal
deposits, but which continue upwards through the whole of the
Bolonian. So on the coast of Dorset the lower limit of the Bolonian
must also be drawn in the midst of clays, where the most marked
introduction of new species commences. This takes place at no very
well defined line; so that the limit must remain open; in any case
it will be below bed No. 29 of:the:Kimmeridge Bay section, and may
be as low as No. 40. At Boulogne,'the ‘‘Middle Portland” has been
taken to end upwards where the sands cease to be marly and are
often consolidated into calcareous grits, the lowest beds of the next
series containing a different fauna, the most remarkable species being
Cardium Pellati. If we draw the same line in England, it will
lie immediately beneath the Flinty series of the coast, the Tisbury
freestone, the Swindon Trigonia-beds, and the rubbly limestones of
Buckinghamshire. In other words, the ‘Portland Sand” must be
thrown into the Upper Bolonian, care being taken that the glau-
conitic and rubbly beds which form the base of the true Portland
are not included. That the sands ought to be separated from the
Portland Stone was perceived by Fitton ; and their distinctness from
the general mass of the Kimmeridge Clay was equally clear to him.
The fact of their containing a fauna much allied to that of the
higher parts of what was then called the Kimmeridge Clay, enables
us rightly to associate the two under a separate and common title,
the Bolonian. This period both in England and the North of
France, served as an introduction to the Portland, with the lowest
beds of which its uppermost strata have several fossils in common.
The localities in England which show Bolonian strata may now
be enumerated. In general, of course, all that has been described
as Portland Sand will now represent part of the Upper Bolonian,
and, in addition, much that has been termed Kimmeridge Clay. The
brick-yards at Upway, the fossiliferous beds at the base of the Tis-
bury section, the sandy “‘ Kimmeridge Clay” of Devizes, so rich in
JURASSIC OF THE PARIS BASIN. 585
fossils, the sandy portions below the actual sand on the northern
slopes of Swindon Hill, the lower part of Shotover Hill with the
finely laminated clays, the uppermost part of the pit at Hly, and the
whole of the mass called Upper Kimmeridge in Lincolnshire’, all
belong to the Bolonian. In most cases no subdivision into Upper
and Lower can be traced; but the record by Prof. Judd (Q.J.G.S.
vol. xxiv. p. 237) of Amm. gigas and Amm. Gravestanus in the ‘‘ Port-
landian ” portion of the Speeton Clay would appear to indicate the
distinctness of the Lower Bolonian in that locality. It appears
from this description that the Upper Bolonian in the northern area
may be divided into 3 minor parts as in the south, viz. the zone of
Cyprina Brongniarti, the zone of Discina latissima, and the Portland
Sands, which last might be called the zone of Belemnites Souichi.
The last series to be considered is the Portlandian. The line of
junction of this with the Bolonian has already been discussed. The
beds above this line which may be certainly placed among Jurassic
deposits, are the Flinty Series, the Building-stones, and the Purbecks
of the Isle of Purbeck. Towards the close of the Jurassic epoch
freshwater conditions appear to have set in in various parts of the
area under study. ‘There is, however, no reason to suppose that
their introduction in every place was synchronous, but every reason
to think the contrary; yet by the custom of calling all these beds
“‘ Purbeck ” their synchronism has been practically affirmed. To
obviate this it is proposed to include the typical Purbecks, as seen in
the Isle of Purbeck itself, in a “ Portlandian ” group, of which it will
form the upper member, while the Flinty series and Building-stones
form the lower. ‘There can be no objection to this, if it renders cor-
relation easier.
It remains, then, only to indicate the localities where these rocks
occur, and their position in the group. In the southern range
no possible representative is met with till we reach Bar-le-Duc,
shortly before entering the Haute-Marne. Here commences a small
mass of rocks formerly considered Suprajurassic, of which the most
noteworthy is the vacuolar oolite. From stratigraphical position, this
might equally well represent the upper part of the Upper Bolonian ;
but the occurrence in it of Astarte rugosa, a characteristic fossil of
true Portland rocks, leads to its being placed as Lower Portlandian,
a correlation to which Pellat (68) agrees (using the term in the
sense now defined). These beds have been proved (40) to be over-
lain unconformably by the Neocomian ; so that nothing higher is to
be found ; but it is a remarkable circumstance that the greatest
development upwards is just at that locality where all detrital beds
are at their maximum, opposite the Straits of Dijon. These beds
soon disappear ; and nowhere else in the same range can similar beds
be found. In the Charente, however, if we correlate the limestones
with Cyprina Brongniarti (or its representative) with the Upper
Bolonian, the succeeding beds with Corbula inflewa must be the base
of the Lower Portland. Indeed the Portlandian and Bolonian may be
* In the map in Quart. Journ. Geol. Soc. vol. xxxi. p. 202, the names ‘“‘ Upper
Kimmeridge” and “‘ Lower Kimmeridge” have been interchanged by error.
586 J. F. BLAKE ON THE UPPER
here less distinct than elsewhere ; for if Coquand is right in recording
OCardium dissimile from the latter, and the shell called Astarte
rugosa has been rightly determined from Chassors, there is a very
Portlandian aspect even about the Lower Limestone, though it would
be impossible, for stratigraphical reasons and from the general cha-
racter of its fauna, to separate it from the Upper Bolonian. Thus
there is nothing to absolutely prevent a geologist from considering,
with Coquand (24), that the gypseous beds at the top belong to the
Upper Portland, ¢.'e. Purbeck ; but it is more in keeping with proba-
bility to regard them as taking the place, without any intervening
gap, of the Lower Portland or true Portland limestone, as Manés
does (17) when he groups the equivalent beds in the Ile d’Oléron
with those below. In the latter locality, at St. Denis, it is undoubted
that beds with Cardium dissimile follow very closely on others with
Cyprina Brongniarts (or its representative) ; and these we are justified
in considering Portlandian. They are followed conformably by the
gypseous beds, which are associated with others containing fossils
like the beds below; and these too, therefore, are placed as Lower
Portlandian. In.the Pays de Bray it has been satisfactorily shown
that above the Upper Bolonian clays come ferruginous grits contain-
ing true Trigona gibbosa; and these are therefore rightly placed
by de Lapparent (69) and Seemann on the horizon of the Lower Port-
landian of the present paper. In the Boulonnais the beds hitherto
called ‘‘Upper Portland” correspond without doubt to the true
Portland limestone, but not to the whole of it. Throughout they
are more or less arenaceous, and correspond lithologically to the
Flinty series, while their characteristic Ammonite is A. bononzensis,
and not A. giganteus, which latter is characteristic of the Building-
stones. Here, therefore, the Portland series is incomplete; and the
beds which lie at the top and contain Astarte socralis and Cyprids
are, for this reason, scarcely likely to represent Purbeck beds. They
are in fact so rubbly and irregular that they cannot be considered
conformable, and may be of any age, either Purbeck or Wealden ;
but there is not the slightest proof that they belong to the former.
Finally, in our own country it has been shown (Q.J.G.8. vol.
xxxvi.) that the Portland limestone is only complete in Dorsetshire
and the Vale of Wardour; and in these two districts the freshwater
(or partially freshwater) strata will belong to the Upper Portlandian,
and be its only representatives. Justifications for a closer associa-
tion of these rocks with the Portland marine limestones than is
allowed by calling them Purbeck, may be found in the occurrence
in them of Hemicidaris purbeckensis in Dorsetshire, a fossil found
also in the Upper Bolonian, and of Trigonia densinoda, belonging
to the Glabrae, recently described by Mr. Etheridge (Q. J.G.S8. vol.
Xxxvil. p. 247) in the Vale-of-Wardour “ Purbecks.” It is true
these beds exhibit local unconformities; but that is natural when
freshwater strata succeed marine; and it is to be noted that “ Pur-
becks” never lie on any thing but “ Portlands.” The so-called
Purbecks of Swindon and those of Buckinghamshire, lying on lower
JURASSIC OF THE PARIS BASIN. 587
portions of the Portland limestones, will belong to the Lower
Portlandian.
In bringing this Part I. to a close, I must not omit to return my
thanks to those who have assisted me ; especially to M. de Lapparent,
who enabled me to study the literature of the subject in Paris, and
who showed me the true Portlandian fossils from the Pays de Bray ;
to Prof. Hébert, who gave me many valuable indications of the best
localities to visit, without which my difficulties would have been
greatly increased ; to M. Rigaux, who has on several occasions guided
me in the Boulonnais; to MM. Cotteau and de Loriol, who have given
me copies of some of their writings for reference; and, finally, to the
Government-Grant Committee of the Royal Society, to whose recom-
mendation I owe the means of carrying on these researches on the
Continent.
EXPLANATION OF PLATE XXVI.
Comparative diagram sections of Upper Jurassic Rocks, Paris Basin
and England.
DiscussrIon.
The Prestprnr stated that the correlations of the author went
far to complete our knowledge of the Upper Jurassic rocks in the
Anglo-Parisian Basin.
Mr. Huptzston was able to confirm the author’s views concerning
the correlation of the Upper Jurassic strata in parts of this country
with those of the Ardennes as regards the lowest beds in question.
The coincidence in the faunas of the beds in these widely separated
areas was very remarkabie. He thought Mr. Blake’s observations
tended to support the views of M. Hébert rather than those of
M. de Loriol with respect to the importance of the Coral Rag as a
formation. He did not agree with the separation of the so-called
“« Pterocerian;” nor could he agree with the author in absorbing the
greater part of the Kimmeridge Clay into his “Bolonian.” The
author’s Bolonian was called by the French authors Lower Portlan-
dian, and was claimed by them as the normal or characteristic de-
posit; while the Portlandian in the south of England, on a higher
horizon, was the less constant development, and therefore more
truly the episode.
Tne AvrHor, in reply to Mr. Hudleston, stated that the Astartian
of this country resembled that of Normandy rather than that of
the Boulonnais; but he agreed with him as to the Pterscerian. He
thought that the calling of the Bolonian by the name of “ Port-
landian” had been a continual source of error.
588 S. S. BUCKMAN ON AMMONITES FROM
39. A Duscriptive CataLoeur of some of the Spucizs of AMMONITES
from the Inrertor Ootire of Dorset. By 8. 8. Buckman, Esq.
(Communicated by James Buckman, Hsq., F.G.8.) (Read
June 22, 1881.)
BEFORE commencing a descriptive catalogue of these Ammonites, it
may be as well to give some idea of the various beds from which
they come. This has been done before ; but, various mistakes having
crept in and new researches having given us fresh information, I
deem it worth while to reintroduce the subject.
The beds under consideration begin with the ‘‘ Sands” or ‘ Pas-
sage-beds,” also called Midford Sands. They are from about 100 to
150 feet, perhaps more, in thickness, with interpolated layers of
comminuted shells about a foot or so thick, occurring at intervals of
from 4 to 10 feet. These layers contain a large conglomeration of
broken shells, so that good specimens are scarce. I have obtained
from them a Rhynchonella which is probably R. cynocephala(Richard.),
besides Harpoceras Moorei (Lycett), and several species of Trigonia
(clavellated and costate), Loma, Astarte, &c.; and I am led to sup-
pose that these sands are probably equivalent to the lower part
of the Cynocephala stage of Lycett, in the Cotteswold Hills.
Above these sands comes the stone of the Inferior Oolite. This
stone changes at certain levels, both in composition, colour, and hard-
ness. The Ammonites do not occur all in one bed, but this Inferior
Oolite stone can be very well divided into four zones, which are ex-
tremely well marked, but vary very greatly in thickness at different
localities; and it is probably this variation in thickness, and some-
times almost complete absence of a zone, that has led to very much
confusion.
At the base of the Inferior Oolite Limestone comes the zone of
Harpoceras Murchisone. It rests on a bed of blue stone, which
probably belongs properly to the sands.
The bed in which H. Murchisone occurs is mostly of a ight brown
colour, sometimes well filled with iron grains, sometimes almost
altogether lacking them; it is generally very hard. At Bradford
Abbas it is about 1 foot thick, but on Corton Down from 3 to 4
feet.
Above this comes the zone of Harpoceras Sowerbyz. ‘This bed is
sometimes light yellow with iron grains, sometimes dark blue with
similar grains, the light yellow being soft and the dark blue hard.
Its range is about 3 feet at Bradford Abbas; and at Halfway House,
&e. it is about the same thickness.
Above this comes the zone of Stephanoceras Humphriesranum,
which is almost entirely, if not quite, absent at Bradford Abbas.
At Oborne, however, its thickness is about 5 feet, while at Louse-
ad
THE INFERIOR OOLITH OF DORSET. 589
Hill and Wyke quarries this zone is only represented by two thin
layers very much charged with iron, the two being only about
6 inches thick, but containing nearly all the species that one finds at
Oborne in the Humphriescanwm-zone.
Above this comes the zone of Cosmoceras Parkinsoni, which varies
very much in different positions. Near Sherborne it is about 15 to
20 feet thick, but very unfossiliferous. At Bradford Abbas it is
about 6 feet thick, the upper part having probably been washed
away; it is rather unfossiliferous. At Clifton Maybank, however,
about 2 miles from Bradford Abbas, a small opening in this zone
was made; and it was found highly fossiliferous, while at Broad
Windsor, and near Bridport, it contains a large number of species and
specimens.
I here give sections of three quarries—one at Oborne, the other
at Wyke, and the third at Bradford Abbas—to show the different
beds clearly.
Fig. 1.—Section at Oborne, near Sherborne.
Zone of Ammonites Parkin- 4
sont.
i
| Light-coloured stone, 2 feet.
bo
Soft sandy stone, 2 feet.
—————-—-~ -—-—
|
Zone of Stephanoceras Hum-
phriesianum,
3 | Harder stone, iron grains, 3 feet.
Sere RS ; ‘
Bed with Spheroceras Sauzei \ 4 White marl, with green grains,
&e. 6 inches.
5 Hard blue and yellow stone, about
| 2 feet.
|
Probably zone of Harpoceras
Sowerbyt.
|
| Unseen.
Bed with Rhynchonella rin- t |
gens. \ |
| Soft yellow sandstone.
590 S. 8. BUCKMAN ON AMMONITES FROM
Fig. 2.—Section at Wyke Quarry.
(
i)
Whitish stone, perhaps 20 feet,
extending up the hill.
Zone of Cosmoceras Parkin- 1
sont. |
Zone of Stephanoceras Hwin- 9 Dark red stone, filled with iron
phriestanum. t __| &e., 7 inches.
f Bluish stone, sometimes yellow,
Zone of Harpoceras Sewer eat 3 with plenty of iron grains,
3 feet 10 inches.
| * HHH X KH ee
| ; Lighter yellow stone, 2 feet.
Zone of Harpoceras Murchi- 4
sone. |
|
Lower part hidden.
Bed No. 2 contains Stephanoceras Humphriesianum, S. Blagdeni, S. Braiken-
ridgui, Cosmoceras Garantianuwm, and many others peculiar to the zone of
Steph. Humphriesianum at Oborne.
xxx Bed with Rhynchonella ringens, Hérault.
Pa
THE INFERIOR OOLITE OF DORSET. 591
Fig. 3.—Section at Bradford Abbas.
{|
ER en assras Parkin- 1 White oolite, 6 feet 6 inches.
soni.
|
|
2 | Marl bed, 3 inches.
Humphriesianum zone. g Bluish stone, 6 inches.
c Wr Trony stone, 6 inches.
|
|
Zone of Harpoceras Sowerbyi. 5 | Vellow atonese f2ck
/
6 | Paving bed, 1 foot.
Zone of Harpoceras Murchi-
HCE Hard blue stone, 1 foot 2 inches.
|
|
|
|
)
|
|
|
|
Perhaps representative of S.- '
(
|
|
(
|
|
Yellow sands. |
Bed No. 4 is perhaps the representative of the Spheroceras-Sauzei bed at Oborne.
Bed No. 2 contains Zerebratula Morieri and Rhynchonella parvula.
The zone of Harpoceras Murchisone in this district contains :-—
Harpoceras Murchison (Sow).
, var. bradfordiense, S. S.
Rhynchonella subangulata, Dav.
Terebratula perovalis, Sow.
Buckm. Waldheimia anglica ( Oppel).
Rhynchonella subtetraedra, Dav. Terebratula Etheridgii, Dav.
subdecorata, Dav., young. | —— simplex, Buckm.
The zone of Harpoceras Sowerbyt contains :—
Harpoceras Sowerbyi (Miller). Lytoceras confusum, 8. S. Buckm.
adicrum ( Waagen). Amaltheus subspinatus, S. S. Buckm.
Levesquei (@ O70.). Astarte excavata, Sow.
fissilobatum (Waagen). elegans, Sow.
—— cornu, 8S. S. Buckm. Terebratula Eudesii, Oppel.
The Spheroceras-Sauzei bed at Oborne contains :—
Spheroceras Sauzei (7 Ord.). Sphzroceras meniscum (Waagen) ?
Stephanoceras polymerum (Waagen). | Harpoceras Sowerbyi (Miller), var.
592 S. S. BUCKMAN ON AMMONITES FROM
The zone of Stephanoceras Humphriesianum contains :—
Stephanoceras Humphriesianum (Sow.). | Stephanoceras Deslongschampsii
Harpoceras cycloides (d’ Ord.). (Defrance).
Cosmoceras subfurcatum (Schloth.). Cosmoceras Caumontii (@’ Orb.).
Garantianum (d’ Oro.). Spheeroceras Wrighti, S. S. Buckm.
Haploceras oolithicum (@ Orb.). Oppelia subcostata, J. Buckman.
Harpoceras Edwardianum (d’Orb.). Ammonites cadomensis, Defrance.
Lytoceras Hudesianum (@’ Orb.). Perisphinctes Davidsoni, S. S. Buckm.
Stephanoceras Blagdeni (Sow.). Terebratula spheroidalis, Sow.,
Stephanoceras Braikenridgii (Sow.). abundant.
linguiferum (d’Ord.). Astarte obliqua, Desh.
Spheeroceras Brongniarti (Sow.). Rhynchonella senticosa, von Buch.
—— Gervillii (Sow.). Terebratula Buckmani, Dav.
This Humphriestanum zone is the * Fossil Bed” in quarries round
Sherborne, where it is so well developed. It has been put down
as the equivalent of the Sowerbyz zone or “ Fossil Bed ” (misleading
term) of Bradford Abbas and neighbourhood under the name of
‘the Cephalopoda bed of the Inferior Oolite ;” and the extraordinary
difference in the species has been attributed to the difference in the
locality.
The fact is that the Humphriestanwm zone is almost absent
at Bradford Abbas, but is represented near Halfway House by a
thin band of ironstone, about 6 inches in thickness, which overlies
the Sowerbyt zone, and which contains a list of species which agrees
with those from the Humphriescanum zone at Sherborne ; while the
Sowerby zone at Sherborne is often not quarried, and therefore has
escaped notice, as it was supposed the quarrymen had reached
the sands, as they do at Bradford Abbas. The term “fossil
bed,” too, was probably answerable for part of the confusion, and
shows the necessity for calling beds by the name of some character-
istic fossil, and not by some local appellation which may often denote
beds at entirely different horizons.
The zone of Cosmoceras Parkinsoni contains :—
Cosmoceras Parkinsoni (Sow.). Stephanoceras zigzag (d’Orb.).
Garantianum (d’Ord.). Terebratula Phillipsi, Morris.
Oppelia Truellii (d@’ Ord.). spheroidalis, Sow.
subradiata (Sow.). Stephani, Dav.
Spheroceras polymorphum (d’O7r9.). Rhynchonella spinosa (Schloth.).
dimorphum (d@ Orb.). Terebratula globata, Sow., variety ?
Perisphinctes Martinsii (@’Ord.).
Besides the Ammonites here mentioned from these four zones, I
have separated about 50 more species, which, so far as | am aware,
have not yet been described. ‘These rocks are also well stocked
with Gasteropoda, of which there are about 150 different species ;
and Lamellibranchiata are very abundant; of Brachiopoda we have
about 40 species made out.
It may be as well before describing the species to explain a few
terms made use of in these descriptions.
The Inner portion of whorl is that which is nearest to the centre
of the Ammonite, otherwise called the dorsal part.
tat racoen
THE INFERIOR OOLITE OF DORSET. 593
Outer portion is the opposite, otherwise called the ventral area.
Shoulder is where the inner portion of the whorl meets the pre-
ceding whorl, and is an important point in the diagnosis of Ammo-
nites ; some shoulders are square, as in Harpoceras Tessonianum
some concave, see Harp. Murchisone ; some convex, some merely
sloping, de.
Termination or mouth-border, i.e. the completion of the body-
chamber.
The termination is variously shaped: some have a plain semi-
lunar band, as Stephanoceras Humphriesianum; others, ears of
various shapes, set up either nearly altogether on the ventral area,
as in Steph. Braikenridgzt, or on the sides and projecting straight, as
in Spheroceras Sauzei (d’Orb.); others have a termination like an §,
as Harpoceras concavum; this is called the double bend; others
have this double bend with a horn projecting from the middle
others have a single bend, like Amaltheus spinatus (Bruguicre).
In the following Tables I have roughly classified the Ammonite
according to their variously shaped terminations :—
1. Semilunar termination.
Stephanoceras Humphriesianum(Sow.).| Stephanoceras Deslongschampsii (De-
Cosmoceras Garantianum (@’ OQrd.).- france).
Stephan. polymerum (Waagen). | Perisphinctes Davidsoni, S. S. Buckm.
2. Semilunar termination, with a deep furrow first, and, sometimes,
a raised lip.
Spheroceras Mansellii, J. Buck.
Spheeroceras Gervillii (Sow.).
dimorphum (d’ Oré.).
Brongniarti (Sow.).
—— Wrightii, SS. Buckm.
3. Spathulate ears, projecting from a little on each side of the
ventral area.
Stephanoceras Braikenridgii (Sow. ys | Perisphinctes Martinsii (D’ Or0.).
Blagdeni (Sow.).
4. Kars like No. 3, but projecting from the side.
Spheeroceras Sauzei (d’ Ord.). | Stephanoceras linguiferum (d’ Ord.).
5. Termination, double bend without any horn.
Harpoceras concavum (Sow.). | Harpoceras cycloides (@’ Ord.).
Murchisonex, var. bradfordiense, adicrum ( Waagen).
S. S. Buckm.
— Moorei (Lyc.).
Haploceras oolithicum (d@’Ord.).
6. Termination, double bend with horn.
Oppelia subradiata (Sow.).
Harpoceras cornu, S. S. Buckin.
Harpoceras Levesquei (d’O7b.).
Cosmoceras Parkinsoni (Sow.) *.
Harpoceras Edwardianum (d’ Orb.).
* T have placed it here on the authority of d’Orbigny’s figures, my own spe-
cimen not showing the termination exactly enough.
Q.J.G.8. No. 148. 2R
O94 Ss. S. BUCKMAN ON AMMONITES FROM
7. Termination like No. 6, but not produced on ventral area.
Cosmoceras subfurcatum (Schloth.). | Cosmoceras Caumontii (d@ Ord.).
8. Termination, a spathulate ear each side, and one on the ventral
are€a.
Ammonites cadomensis, Defrance.
9. Termination, a plain single bend, more or less produced on
ventral area.
Amaltheus spinatus (Brugwiére) in the Lias.
Inf. Oolite. Amaltheus subspinatus, S. S. Buckm.
Lytoceras confusum, S. S. Buckm.
We will now proceed to give a short notice of the various species
of Ammonites recognized in this district.
STEPHANOCERAS HuMPHRIESIANUM (Sow.).
1825. Ammonites Humphriesianus, Sow. Min. Conch. pl. 500,
middle figure.
1830. A. Humphriesianus (Sow.), Zieten, Petref. pl. 67. fig. 2.
1845. A. Humphriesianus (Sow.), d’Orb. Pal. Franc. Terr. Jurass.
pls. 133, 134, 185. figs. 1, 2.
1849. A. Humphriesianus (Sow.), Quenstedt, Ceph. tab. 14.
figs. 7, 11; Quenstedt, Jura, pl. 54. figs. 2, 3, 4.
1849. A. coronatus oolithicus, Quenstedt, Ceph. tab. 14. fig. 4.
1856. A. Humphriesianus (Sow.), Oppel, Juraformation, p. 376,
no. 40.
1856. A. subcoronatus, Oppel, Juraformation, p. 376, no. 39.
1856. A. Bayleanus, Oppel, Juraformation, p. 377, no. 43.
1854. A. Humphriesianus (Sow.), Morris, Catalogue, p. 292.
1878. Stephanoceras Humphriesti (Sow.), Bayle, Explic. de la
Carte Géol. de la France, vol. iv. pl. 51, figs. 2, 3.
1881. A. Humphriesianus (Sow.), J. Buckman, Quart. Journal
Geol. Soc. vol. xxxvii. p. 65, fig. 6.
Bayle in ‘ Explication de la Carte Géologique de la France,’ vol.
iv. plate 51. figs. 2, 3, shows what I take to be a rather peculiar
variety of Stephanoceras Humphriesianum.
Locahittes. Oborne, and near Sherborne, Burton Bradstock, and
other places: rather common.
Quenstedt, under the name of Amm. coronatus oblithicus, figured the
young form of the thick variety of this species, which Oppel also
mentioned by the name of subcoronatus. Oppel also separated the
thin form, under the name of Bay/eanus, observing that it occurred
lower than Humphriesianus proper. My own observations, however,
do not agree with this, as I have found both the thin and thick
varieties together; and Mr. D. Stephens assures me that they both
occur together at Milborne Wick, the thin variety being the com-
moner. I have, however, seen the necessity for distinction, and
have kept Oppel’s names for the varieties, the thick variety being
Stephan. Humphriesianum, var. subcoronatum (Oppel), and the thin
Stephan. Humphriesianum, var. Bayleanum (Oppel).
THE INFERIOR OOLITE OF DORSET. 595
SrEPHANOCERAS DxEstonescHampsit (Defrance).
1845. Ammonites Deslongschampsi (Defr.), d’Orb. Terr. Jurass.
pl. 138. figs. 1, 2
1856. A. Deslongschampsu (Defr.), Oppel, Juraform. p. 378,
no. 44.
1880. Stephanoceras Deslongschampsu (Defr,), Wright, Lias Amm.
Palzont. Soc. 1880, p. 224, fig. 116.
Locality. Humphriesianum zone, Oborne: very rare.
The termination of this species is a fine semilunar border. One
beautiful specimen showing this was obtained from Oborne by E.
Cleminshaw, Esq., F.G.S.
SrEPHANOCERAS BragpENt (Sow.).
1818. Ammonites Blagdent, Sow. Min. Conch. pl. 201.
1818. A. Banks (Sow.), Min. Conch. pl. 200.
1830. A. coronatus (Schloth.), Zieten, Verstein. Wirttemb. tab. i.
fig. 1.
1845. A. Blagdeni (Sow.), @Orb. Terr. Jurass. tab. 132.
? A. coronatus, Quenstedt, Der Jura, tab. 51. fig. 1.
1849. ? A. coronatus, Quenstedt, Ceph. tab. 14. fig. 1.
1854. A. Blagdeni (Sow.), Morris, Catalogue, p. 290.
A. Blagdent (Sow.), Morris and Lycett, Great Ool. Moll.
tab. 14. fig. 3.
1856. A. Blagdeni (Sow.), Oppel, Juraformation, p. 374, no. 38.
1880. Stephanoceras Blagdent (Sow.), Wright, Lias Ammonites,
Palzont. Soc. 1880, p. 251, figs. 157, 158.
Localities. This species occurs in the Humphriesianum zone of
Oborne, Sherborne, &e. |
Stephan. (Ammonites) Banksii (Sow.) is merely a very large
variety of this species.
STEPHANOCERAS BRAIKENRIDEII (Sow.).
1818. Ammonites Braikenridgui, Sow. Min. Conch pl. 184.
1845. A. Br OAL (Sow.), @Orb. Terr. Jurass. pl. 135.
figs. 3-5.
We Braikenridgu (Sow.), Quenstedt, Der Jura, tab. 54. fig. 5.
A. Braikenridgit (Sow.), ? Morr. & Lyc. Great Ool. Moll. pl. 14.
fig. 1.
” 1854. A. Braikenridgii (Sow.), Morris, Catalogue, p. 290.
1856. A. Braikenridgiu (Sow.), Oppel, Juraformation, p. 377,
no. 42.
1880. Stephanoceras Braakenridgu (Sow.), Wright, Lias Ammo-
nites, Palzont. Soc. p. 251, figs. 159, 160.
1881. A. Braikenridqu (Sow. ), J. Buckman, Date Journ. Geol.
Soc. vol. xxxvii. p. 62, fig. 3.
Localities. Humphriesianum zone at Oborne, and othise quarries
near Sherborne.
The termination of this species is a fine ear on each side, as is
well shown in @’Orbigny. The length of ears varies very much;
2R 2
596 S. 8S. BUCKMAN ON AMMONITES FROM
and I have some specimens which very much resemble Steph.
Humphriesianum, var. subcoronatum (Oppel), both in the number of
ribs and in other respects, but have short ears.
STEPHANOCERAS LINGUIFERUM (d Orb.).
1845. Ammonites linguiferus, d’Orb. Terr. Jurass. pl. 136.
1856. A. linguiferus (d’Orb.), Oppel, Juraform. p. 376, no. 40.
Locality. Zone of Stephan. Humphriesianum at Oborne: very
rare.
I possess one specimen with the termination ; it has a small plain
ear projecting from the side.
STEPHANOCERAS ziezaé (d’Orb.).
1845. Ammonites zigzag, d’Orb. Pal. France. pl. 129. figs. 9,
MO, Wk
1856. A. zigzag (d’Orb.), Oppel, Juraformation, p. 378, no. 45.
Of this species there are two forms, a thick and a thin one. They
are found, however, in the same bed in the same localities, and are
similar in all other respects.
The thick primary ribs, so conspicuous in the small specimens,
gradually disappear as the fossil becomes larger, and give place to
small rounded primary ribs, which come much closer together, some-
times dividing into secondary ribs, and sometimes passing straight
round the ventral area without dividing at all.
Localities. Parkinsoni zone at Broad Windsor, Crewkerne Sta-
tion, &e.
I have no specimen with the termination ; but the body-chamber
is very long, as I possess one specimen with a body-chamber nearly
one whole whorl in length, and yet it does not show even a sign
of the termination.
STEPHANOCERAS POLYMERUM (Waagen).
1867. Ammonites polymerus, Waagen, Geogn. Pal. Beitrage,
p- (99) 605.
1845. A. Brongmarti, VOrb. (non Sowerby), Terr. Jurass. pl. 137.
figs. 1, 2.
1881. A. Brong gmart, J. Buckman (non aa Quart. Journ.
Geol. Soc. vol. xxxvii. p. 64, fig. 5.
Locality. This species occurs at Oborne, in a whitish sort of
marl, with Spheroceras Sauzet.
In the young state it very much resembles the thin form of
Stephan. Humphriesicanum; but when adult it is far more like a
Spheeroceras.
Spymroceras Savuzer (d’Orb.).
1845. Ammonites Sauzei, d’Orb. Terr. Jurass. tab. 149.
1856. A. Sauzei (d’Orb.), Oppel, Juraformation, p. 375, no. 37.
1867. A. Sauzec (d’Orb.), Waagen, Geogn. Paldont. Beitrage,
p- (100) 606.
THE INFERIOR OOLITE OF DORSET. 597
1878. Spheroceras contractum, Bayle (non:Sowerby), Explication
de la Carte Géol. de la France, vol. iv. pl. 53. figs. 1, 2.
1881. A. Sauzec (VOrb.), J. Buckman, Quart. Journ. Geol. Soc.
vol. xxxvil. p. 62, no. 6.
Localities. Marly bed below the zone of Stephan. Humphriesianum
at Oborne and near Sherborne: rather scarce.
SpH#=ROcERAS Bronenrarri (Sow.).
1817. Ammonites Brongniarti, Sow. Min. Conch. tab. 184 a. fig. 2.
1845. A. Gervilliz, dV’ Orb. (non Sow.), Terr. Jurass. pl. 140. figs. 3-8
(non 1, 2, non Sowerby).
1849. A. Brongniarti (Sow.), Quenstedt, Ceph. tab. 15. fig. 9.
1856. A. Brongniarti (Sow.), Oppel, Juraform. p. 375, no. 35.
1867. A. Brongniarti (Sow.), Waagen, Geogn. Pal. Beitriige,
p- (96) 602.
1878. Spheroceras Brongniarti (Sow.), Bayle, Explic. de la Carte
Géologique de la France, pl. 53. figs. 3, 4, 5.
Localities. Humphriesianum zone at Oborne, near Sherborne, &c.
Rather common.
The species that I have placed under this name is the one figured
by Sowerby with the closed umbilicus ; and the other I have called
Spher.Gervillii. I do this because most authorities have so taken it ;
d’Orbigny, however, transposed them, whether rightly or not I am
unable to say without seeing Sowerby’s original specimens. There
seems to have been some misprint or confusion with regard to them
in Sowerby’s work.
SPH#ROCERAS GERVILLII (Sow.).
1817. Ammonites Gervilli:, Sow. Min. Conch. pl. 1844. fig. 3.
1849. A. Gervillu (Sow.), Quenstedt, Ceph. tab. 15. fig. 11.
1856. A. Gervillit (Sow.), Oppel, Juraform. p. 375, no. 36.
1867. A. Gervillu (Sow.), Waagen, Geogn. Palaont. Beitrage,
p- (99) 605.
1878. Spheroceras Gervilla (Sow.), Bayle, Explic. de la Carte
géologique de la France, pl. 53. figs. 6, 7.
1881. A. Gervillii (Sow.), J. Buckman, Quart. Journ. Geol. Soc.
vol. xxxvil. p. 63, fig. 4.
Localities, Humphriesianum zone at Oborne, near Sherborne, &c.
Not so common as Spher. Brongnarti.
SPH HROCERAS MENISCUS (Waagen) ?
1867. Ammonites meniscus, Waagen, Geogn. Paliont. Beitrage,
p- (96) 602.
1875. A. Gervillii, d’Orb. pars (non Sowerby), pl. 140. figs. 1, 2.
Mr. E. Cleminshaw found one specimen at Oborne in the Sauzei
bed, which I have referred to this species.
SpuHz@rRoceras Mawsetiir (J. Buckman).
1881. Ammonites Mansellii, J. Buckman, Quart. Journ. Geol.
Soc. vol. xxxvil. p. 64, no. 18.
598 S. 8. BUCKMAN ON AMMONITES FROM
This species, when young, is extremely like Spher. Brongniarti
(Sow.), plate 184 a. fig. 2, but when larger is easily distinguished
by its very fine and numerous bifurcating ribs and its very square
ventral area, especially just by the termination, and its far greater
breadth. It also attains a larger size than Spher. Brongniarti. The
termination is also peculiar—first a small lip, then a deep furrow,
then another lip and band.
This species was named but not figured by Mr. J. Buckman in
his paper read before the Geological Society.
Dimensions. Diameter 1°75 inch; umbilicus 0°33; aperture
across 1:20; aperture back to front 0°45.
Locality. Clatcombe, near Sherborne. Two fine specimens were
obtained from this place by T. C. Maggs, Esq. I do not know of
any other specimens.
SPHHROCERAS POLYMORPHUM (d’Orb.).
1845. Ammonites polymorphus, @Orb. Terr. Jurass. pl. 124. figs.
1, 2, 3, 4, 5? 6?
1849. A. Parkinsoni inflatus, Quenstedt, Ceph. Tab. iu. figs.
6 and 7.
1854. A. polymorphus (d’Orb.), Morris, Catalogue, p. 294.
1856. A. polymorphus (d’Orb.), Oppel, Juraform. p. 382.
We have undoubtedly found in this neighbourhood specimens
which exactly correspond with those figured by d’Orbigny, ‘ Ter-
rains Jurassiques,’ pl. 124. figs. 1, 2, 3,4; but we have not found
any to correspond with figs. 5 and 6; and I have my doubts about
figs. 5 and 6 really being the adult form of the others. Oppel, too,
in quoting A. polymorphus, d’Orb., leaves out nos. 5 and 6 (see
Oppel, ‘ Juraformation,’ p. 382, no. 54).
Localities. Zone of Cosmoceras Parkinsoni at Broad Windsor, Bur-
ton Bradstock, and other places.
SPH#ROCERAS DIMORPHUM (d’OrD.).
1845. Ammonites dimorphus, dOrb. Terr. Jurass. pl. 141.
1854. A. dimorphus (d’Orb.), Morris, Catalogue, p. 291.
This species varies somewhat in the width of its umbilicus. Some
specimens have the umbilicus nearly closed, while others of the same
size have the umbilicus much larger, so that a portion of the
inner whorls can be seen.
In the adult form the umbilicus widens rather quickly, as is
well shown by d’Orbigny, pl. 141. fig. 1.
The variety represented by d’Orbigny (pl. 141. figs. 3 and 4)
has, so far as I know, not yet been obtained from this district.
I possess only one specimen with the termination. It is a
form with a rather wide umbilicus. The termination is merely
a small furrow and a semilunar lip beyond. The specimen came
from Bradford Abbas.
Localities. Zone of Cosmoceras Parkinsont at Halfway House,
Broad Windsor, Stoford, and other places.
THE INFERIOR OOLITE OF DORSET. 599
Spom{RocerRAS Wrieutir, S. 8. Buckman, n. sp.
1849. Ammonites microstoma, Quenstedt (non dOrbigny), Cepha-
lopoda, tab. 15. fig. 6..
Localities. Humphriesianum zone, Oborne, and near Sherborne:
common. ;
This species was figured by Quenstedt under the name of A. au-
crostoma; but it does not at all agree with the figure of A. micro-
stoma given by d’Orbigny (who named it) in ‘ Terr. Jurassiques.’
Dimensions. Diameter, adult, 1°59 inch; umbilicus 0:55 inch;
umbilicus, omitting the last chamber, 0°22 inch; breadth, same
place, 0°85 inch; breadth across termination 0°79 inch; termina-
tion, from back to front, 0°50 inch.
Length of body-chamber very nearly one whole whorl.
Named in compliment to Dr. Wright, of Cheltenham, who is so
ably working at the Lias Ammonites.
Cosmocrras Parxinsont (Sow.).
1821. Ammonites Parkinsoni, Sow. Min. Conch. pl. 307.
1845, A. Parkinsoni (Sow.), d’Orb. Ter. Jurass. pl. 122, variety.
1849. A. Parkinson gigas, Quenstedt, Ceph. tab. ii. fig. 1 (adult
form).
1854. A. Parkinson (Sow.), Morris, Catalogue, p. 294.
1856. A. neuffensis, Oppel, Juraformation, p. 378, no. 48.
1856. A. Parkinsoni (Sow.), Oppel, Juraformation.
1849. A. Parkinsoni depressus, Quenstedt, Ceph. tab. i. fig. 5.
1878. Parkinsonia Parkinsoni (Sow.), variety, Bayle, Exp. de la
Carte géol. de la France, vol. iv. pl. 67. figs. 2, 3.
1878. Parkinsonia neuffensis, Bayle ?, pl. 67. fig. 1.
This species is somewhat variable, and has been much misunder-
stood. The figures given by d’Orbigny (‘ Terr. Jurass.’ pl. 122. figs. 1
& 2) are evidently of a variety of Sowerby’s species. This same
variety is again figured by Quenstedt under the name of A. Par-
kinsont depressus ; and as such it was quoted by Oppel (‘ Juraforma-
tion’) as asynonym for Parkinson. It was also figured by Bayle
under the name of Parkinsonia Parkinsoni (see synonyms).
This variety differs from Sowerby’s type in having far fewer ribs, far
less inclusion (consequently the whorls are not so broad from front
to back), and in possessing rather marked tubercles.
To this variety I give the name of Cosmoceras Parkinsoni, var.
rarecostatum, 8. S. Buckman.
The fragment figured by Quenstedt (Ceph. tab. ii. fig. 1) under
the name of Ammonites Parkinsoni gigas is merely the very adult
form of the true Parkinsoni; and this adult form occurs at Half-way
House of very large size, one specimen measuring 19 inches across,
and yet lacking a large portion of the outer chamber. This adult
form was named by Oppel Ammonites neuffensis, he giving Quen-
stedt’s figure as a reference. Bayle has also figured a specimen as
Am. neuffensis ; but I consider that his figure most probably repre-
sents merely a rather fine-ribbed variety of a medium-sized true
C. Parkinsons.
600 S. S. BUCKMAN ON AMMONITES FROM
The true C. Parkinsoni occurs in great numbers at Halfway House,
also at Bradford Abbas, Burton Bradstock, and Sherborne.
The variety rarecostatum, 8. 8. Buckm., occurs in the same beds
at Sherborne, Bradford Abbas, Burton Bradstock, Broad Windsor,
&c., but is not so common.
Cesmoceras Parkinsoni is characteristic of the upper beds of the
Inferior Oolite. The very adult forms lose all their ribs and also
the division on the ventral area, and are very different from the
ordinary young form which was figured by Sowerby.
Bayle has separated this species from the genus Cosmoceras under
the generic name of Parkinsonia. I am rather of opinion that it,
and also Cosm. Caumontu (d’Orb.), should be so separated.
The termination of this species is somewhat produced on the ven-
tralarea. I possess one specimen with the termination on the outer
half of the whorl well shown, but am unable to say whether the
species possesses a horn on the side, or merely a plain double curve.
Length of body-chamber = of a whorl.
Cosmocrras Caumontit (d’Orb.),
Ammontes Caumontu, @Orb. Terr. Jurass. pl. 138. figs. 3, 4.
Locality. It occurs at Oborne in the zone of Stephan. Humphriesi-
anum, but 1s scarce.
The termination is merely a small, very thin, narrow ear.
Cosmoceras GaRantranum (d’Orb.).
1845. Ammonites Garantianus, @Orb. Terr. Jurass. pl. 123.
1849. A. Parkinsoni dubius, Quenstedt, Ceph. tab. ii. fig. 9.
1854. A. Garantianus (d’Orb.), Morris, Catalogue, p. 292.
1856. A. Garantianus (d’Orb.), Oppel, Juraformation, p. 381,
no. 93.
Localities. Humphriesianum zone, and less commonly in the lower
part of the Parkinsona zone, Oborne, Louse Hill, Wyke: rather
common.
The termination is a semilunar band.
CosmocERAS suBFURCATUM (Schlotheim).
1830. Ammonites subfurcatus (Schlotheim), Zieten, Verst. Wiurt-
temb. pl. vii. fig. 6.
1845, A. niortensis, d’Orb. Terr. Jurass. pl. 121. figs. 7-10.
1849. A. Parkinsons bifurcatus, Quenstedt, Ceph. tab. 11. fig. 11.
1856. A. subfurcatus (Zieten), Oppel, Juraform. p. 381, no. 52.
Zicten figures this species, giving Schlotheim as the authority for
the name.
Zieten’s figure shows a fossil witha large number of bifurcating
ribs, which is the exception and not the rule, this species usually
having very few bifurcating ribs, as is shown by d’Orbigny, who
figured it under the name of A. mortensis.
[There is also a fossil, of which a few specimens have occurred
at Oborne, which is probably a variety of this species. It has very
THE INFERIOR OOLITE OF DORSET. 601
much the shape &c. of Cosmoceras subfurcatum, and is ornamented
with four rows of sharp spines, Just where they occur in Cosm.
subfurcatum ; but it is entirely destitute of ribs. |
Locality. Higher part of the Humphriesianum zone at Oborne.
The termination is a spathulate ear, slightly wider towards the
extremity.
Morris, in his Catalogue, put this species down as a synonym
of Cosmoceras Parkinson; but it is quite distinct from it, espe-
cially in its mode of volution. It also occurs lower, viz. in the
zone of Stephan. Humphriesianum.
Lytocrras Evpsstanum (d’Orb.).
Ammonites Hudesianus, d’Orb. Terr. Jurass. pl. 1238.
A, Hudesianus (d’Orb.), Quenstedt, Der Jura, tab. 54. fig. 8.
A, Eudesianus (d’Orb.), Oppel, Juraformation, p. 373, no. 29.
This species was for a long time put down for the Inferior
Oolite of this district by the name of A. cornucopiw, Young.
Locality. It occurs in the zone of Stephan. Humphriesianum at
Oborne, but is rare.
LytocrRas ToRULOSUM (Schubler) ?
Ammonites torulosus (Schibler), d@Orb. Terr. Jurass. pl. 102.
figs. 1, 2.
I have one fragment from the sands near Bridport, but am not
quite certain if it belongs to this species.
Lytoceras conrusum, 8. 8. Buckman, n. sp.
Syn. ? Ammonites jurensis, Morris, Catalogue, p. 292.
This species approaches nearly to Lytoceras jurense (Zieten), and
has been quoted from this district under that name. It, however,
differs from it in a great number of points—namely, the shape of
the aperture, which is nearly trianglar, in the very square shoulder,
in the number of whorls, and the lobes, which are more compli-
cated than in L. jurense (Zieten). Inclusion is small. The test
is quite plain, but hasafew marked lines of growth in the young
form, which also has not the peculiar square shoulder much marked.
In occurs in the Sowerbyi zone at Bradford Abbas, Halfway
House, Bradford Abbas railway-cutting, &c.
At Half-way House the specimens are of an enormous size, one
measuring as much as 17 inches in diameter.
The species is somewhat abundant; but small specimens are very
rare.
[ have one small specimen, from Bradford Abbas, with the ter-
mination. It is a plain bend forward towards the ventral area.
Dimensions. Young form, diameter 1:25 inch; umbilicus 0:43
inch; aperture, length 0-47 inch, breadth 0-40 inch ; inclusion about
0:03 inch.
Adult form, diameter 15:90 inches ; umbilicus 7-20 inches ; aper-
602 S, 8S, BUCKMAN ON AMMONITES FROM
ture, back to front, 4:50 inches, across about 53 inches, inclu-
sion 0-80 inch.
The aperture is, as nearly as possible, an equilateral triangle
with a small piece out, caused by the inclusion. The ventral area,
however, is a good deal rounded.
PrRISPHINCTES PYemmuM (d’Orb.).
Ammonites pygmeus, d’Orb. Terr. Jur. pl. 129. figs. 12, 13.
I have one specimen of this species from the neighbourhood.
PerispHinctes Marrtinsit (d’Orb.).
1845. Ammonites Martins, d’ Orb. Terr. Jurass. pl. 125.
1854, A. Martinsa (d’Orb.), Morris, Catalogue, p. 293.
1856, A. Martinsic (d’Orb.), Oppel, Juraformation, p. 387.
Localities. Lone of Cosmoceras Parkinsoni at Halfway House,
Bradford Abbas, Sherborne, and Burton Bradstock, but is rather
scarce.
[At Oborne, in the Yumphriesianum zone, we find a very thin flat
Ammonite with the furrows well marked. It is far more involute
than Perisphinctes Martinsii, the amount of involution being nearly
half the preceding whorl. It has a semilunar mouth-border, which
projects well forward on the ventral margin.
It has hitherto been put down as the same as P. Martinsw; but
I feel certain that it should be separated as distinct from it, both on
account of its stratigraphical position and also its lobes and other
features. I propose forit the name Perisphinctes Davidsont, in com-
pliment to Thos. Davidson, Esq., F.R.S. |
Ihave one specimen of Perisph. Martinsii, d’Orb., with the termi-
nation. It has two long ears, the inner edges of which project well
forward till they touch the inner whorl. This termination is well
represented by d’Orbigny, Terr. Jurass. pl. 125. fig. 1. The termi-
nation represented in fig. 3 may possibly have been taken from a
specimen of Perisph. Davidsoni, 8.8. Buckm.
Harpoceras Sowrrsyt (Miller).
1821. Ammonites Sowerbyr (Miller), Sow. Min. Conctt tab. 213.
1821. A. Brown, Sow. Min. Conch. tab. 263. figs. 4, 5.
1845. A. Sowerby: (Miller), var., d’Orb. Terr. Jurass. pl. 119.
1849. A. Sowerbyi_(Miller), Quenstedt. Ceph. p. 374.
1854. A. Sowerbyz (Miller), Morris, Catalogue, p. 295.
1867. A.Sowerbyi (Miller), var., Waagen, Geogn. Palaont. Beitriige,
pl2ie ties 2.
1856. A. Sowerby: (Miller), Oppel, Juraformation, p. 369, no. 20.
The figure given by d°Orbigny, pl. 119, represents a variety of
this species, and it differs from it in several points. Waagen has
also figured, pl. 27. fig. 6, a peculiar variety.
Localities Ke. Harpoceras Sowerbyt is a scarce fossil, the species
which has been put down by that name as occurring in this district
being really Harp. adicrum (Waagen). ‘The chief characteristics of
Harp. Sowerbyt are a very large keel, and sides which slope in gra-
THE INFERIOR OOLITE OF DORSET. 603
dually to join the inner whorl. It occurs at Sherborne and Bradford
Abbas, but is rare.
The variety figured by d’Orbigny occurs at Bradford Abbas, but
is also rare.
HARPOcERAS ADICRUM (Waagen).
1867. Ammonites adicrus, Waagen, Geogn. Pal. Beitrage, pl. 25.
hie. 7.
Localities. Zone of Harpoceras Sowerbyi at Bradford Abbas, Half-
way House, Louse Hill, and many other places; rather abundant.
This species often attains a very large size.
Dr. Waagen has very properly separated this species from Harpo-
ceras Sowerby2 (Miller). It is sometimes rather difficult to separate
it from some of the varieties of that species; but it is really distinct
In possessing a small rounded keel, as opposed to the large sharp
one of Harp. Sowerbyt, also a larger umbilicus and large distinct ribs,
when adult, at a time when Harp. Sowerbyi is smooth.
H4RPOCERAS FISSILOBATUM (Waagen).
Ammonites fissilobatus, Waagen, Geogn. Pal. Beitrige, pl. 27.
ie, db
Locality. This species occurs at Sandford-Lane quarry near Sher-
borne. I believe it is in the zone of Harpoceras Sowerbyi; but I
have never seen this quarry worked. It is a common fossil there.
HARPOCERAS CONCAVUM (Sow.).
1812. Ammonites concavus, Sow. Min. Conch. pl. 94. fig. 2.
1881. A. concavus (Sow.), J. Buckman, ‘“‘ Terminations of Ammo-
nites,” Quart. Journ. Geol. Soc. vol. xxxvii. p. 60, fig. 1.
Localities. This species is common in the Sowerbyt zone at Brad-
ford Abbas, Halfway House, Sherborne, &c.
The termination is a curve like an §; that is, it rises from the
inner whorl, curving forward, then rounded and curving back, and
then produced on the ventral area. It has no horn, as was sup-
posed when it was figured in the Geological Journal. The species
that d’Orbigny has figured by this name (Terr. Jurass. pl. 116)
does not seem to me at all to agree with Sowerby’s figure.
Harrocreras Murcutson x (Sow.).
1829. Ammonites Murchisone, Sow. Min. Conch. tab. 550.
1825. A. corrugatus, Sow.? Min. Conch. tab. 451. fig. 3.
1830. A. Murchisone (Sow.), Zicten, Verstein. Wirttemb. tab. vi.
1845. A. Murchisone (Sow.)?, d’Orb. Terr. Jurass. pl. 120. figs. 1,
7. Be, Ville ts
1854. A. Murchisone (Sow.), Morris, Catalogue, p. 293.
1856. A. Murchisone (Sow.), Oppel, p. 368, no. 18.
1867. A. Murchisone (Sow.), Waagen, Gevogn. Pal. Beitrage, p.(92)
598, § 31.
1878. Ludwigia Murchisone (Sow.), Bayle, Carte. Géolog. de la
France, pl. 85.
604. S. S. BUCKMAN ON AMMONITES FROM
Localities. This species marks a distinct zone, which is just on the
top of the sands or passage-beds. This zone is about a foot thick at
Bradford Abbas, but about 3—4 feet at Corton and Hawthorn Downs.
Harpoceras Murchisone occurs at Bradford Abbas, Marston Road,
Corton and Hawthorn Downs, and other places, and also rather
plentifully, but badly preserved, at Haselbury.
There is a variety(?) which I am inclined to think should be
separated from Harp. Murchisone. It has a smallish umbilicus and
very fine ribs, and is far thinner. I have given it the name of
Harpoceras Murchisone, var. bradfordiense, 8.8. B.
Dimensions of a medium-sized specimen of Harp. Murchisone :—
Diameter 2°85 inches, umbilicus 0°96, breadth of aperture 0°70 ;
outer whorl, back to front, 1:20 inch.
HARPOcERAS CycLorpus (d’Orb.).
1845. Ammonites cycloides. @Orb. Pal. Frang. Terr. Jurass. pl. 121.
figs. 1-6.
1856. A. cycloides (d’Orb.), Oppel, Juraformation, p. 370.
1867. A. cycloides (d’Orb.), Waagen, Geogn. Pal. Beitriige , Pp. (92)
598.
Localities. Humphriesianum zone at Oborne and quarries near
Sherborne, somewhat plentiful; also at Wyke Quarry, but scarce.
A variable species, some specimens being very thick, with a small
umbilicus and coarse ribs, and others thin, with larger umbilicus and
smaller ribs. The two varieties, however, merge one into the other.
D’Orbigny has well represented the two extreme forms.
This species was formerly quoted by the name of Amm. Cado-
mensis, on account of the misprint underneath d’Orbigny’s plate.
Harpoceras Levesquai (d’Orb.)?
Ammonites Levesque, @Orb. Terr. Jurass. pl. 60 (misprinted
solaris, Phillips).
I quote this species with some hesitation, as our specimens seem
to have fewer whorls and somewhat more marked ribs.
Our specimens are from the zone of Harpoceras Sowerbyi at Brad-
ford Abbas, Halfway House, &c. ; not very common.
Harpoceras Epovarpranum (d’Orb.) ?
1845. Ammonites Edouardianus, d’Orb. Terr. Jurass. pl. 180. figs.
3-5.
1856. A. Hdouardianus (d’Orb.), Oppel, Juraformation, p. 370.
1881. A. Edouardianus (d’Orb.), J. Buckman, Quart. Journ. Geol.
Soc. vol. xxxvii. p. 61, no. 3.
Our specimens do not seem to agree very well with d’Orbigny’s
figures, and are perhaps not the same. They have a more open
umbilicus and far less inclusion; consequently the whorls are less
QCross.
Locality. Humphriesianum zone at Oborne: scarce.
THE INFERIOR OOLITE OF DORSET. 605
HARPOCERAS DISPANSUM (Lycett).
My authority for this name is a specimen sent by Dr. Lycett,
labelled “* Am. dispansus, Lyc., Frocester Hill.”
I have one specimen from near Crewkerne which agrees very well
with it.
Harpoceras Mooret (Lycett).
Ammonites Moorer, Lyc. Cotteswold Hills, pl. 1. fig. 2.
A, Moorei (Lyc.), J. Buckman, Quart. Journ. Geol. Soc. vol. xxxvil.
p- 65, fig. 7.
Localities. Found in layers of comminuted shells in the sands at
Bradford Abbas, Yeovil Junction, &c.: not very common.
Termination. A slight double curve produced on the ventral area.
Harpoceras cornu, 8. 8. Buckman, n. sp.
Ammomites subradiatus, J. Buckman (non Sowerby), “Terminations
of Ammonites,” Quart. Journ. Geol. Soc. vol. xxxvii. p. 61, fig. 2.
This species is compressed, with strongly marked ribs, which are
slightly reflexed and not so prominent close to the termination.
They seldom bifurcate; but now and then a rib comes in between
which is not continued all across.
Keel distinct, with very sloping sides.
Aperture sagittate.
The umbilicus varies somewhat in width; it is, however, rather
wide, with strongly marked ribs, showing also a certain portion of
each whorl.
Shoulder concave.
Termination. Like that of Harpoceras concavum (Sow.); but it has
a very long horn on each side.
Difference. This species resembles Harp. concavum, but is distinct
on account of the horn which the termination possesses, and which I
I have never seen in that species. The ribs are also far more
marked, and the umbilicus is far wider.
This species never attains the same size as H. concavum; but very
small specimens of these two species are hard to separate.
This species might possibly be mistaken for the young of Harpo-
ceras Murchisone (Sow.); it, however, never attains the size of
H. Murchisone, is found at a higher level, has a more prominent
keel, is far thinner towards the keel, is more acute, and its ribs are
less prominent and rather more rounded.
Dimensions. Diameter 2°50 inches, umbilicus 0:60, breadth of
aperture 0°48, outer whorl from back to front 1°15. Another spe-
cimen measured—diameter 2°70 inches, umbilicus 0°82, breadth of
aperture 0°50, outer whorl from back to front 1:06, length of
_horns 0°65.
IT have never seen a specimen of this species which exceeded the
diameter of about 22 inches.
Compare these measurements with those of a medium-sized Harp.
Murchisone (Sow.).
606 S. S. BUCKMAN ON AMMONITES FROM
Remarks. This species was figured in the ‘Quarterly Journal of
the Geological Society ’ for February 1881, under the name of Am-
monites subradiatus ; but it is very distinct from that species, the
umbilicus alone being sufficient to distinguish it.
Localities. It is found in the zone of Harpoceras Sowerbyi at
Bradford Abbas, Halfway House, and many other places. It is
tolerably common.
AMALTHEUS SUBSPINATUS, S. S. Buckman, n. sp.
This species is so peculiar and distinct from all others which I
have met with in the Inferior Oolite, that I think it worth while to
mention it here, although it has not been figured.
It is very nearly allied to Amaltheus spinatus (Bruguiere) of the
Marlstone. It possesses the peculiar crenulated keel, which is dis-
tinct; but the crenulations are not very prominent. It has a large
number of whorls, and very small inclusion, but does not increase in
breadth at all rapidly. It has many fine angular ribs, ornamented
With two spines on each rib, one set being in much the same place
as those on Amaltheus spinatus, while the other set is on the inner
portion of the whorl.
Aperture. Quadrangular.
Dimensions. Diameter 3 inches, umbilicus 1°55, aperture from
back to front 0-75, across 0°67, inclusion barely any.
Localities. It occurs in the Sowerbyt zone at Bradford Abbas,
Halfway House &c., but is scarce.
The termination is like that represented by d’Orbigny(Terr. Jurass.
pl. 52. fig. 1) for Amaltheus spinatus—a plain single bend, much
produced on the ventral area.
OppEtia T'RUELLI (d’Orb.).
1845. Ammonites Truellii, dOrb. Terr. Jurass. pls. 117, 129.
figs. 1, 2.
1849. A. Truellii (V’Orb.), Quenstedt, Jura, tab. 54.
1854. A. Truellic (d’Orb.), Morris, Catalogue, p. 295.
1878. Oppelia Truellai (d’Orb.), Bayle, Géologie de la France,
vol. iv. pl. 89. figs. 1, 3, 4 (2?, 52).
Occurs in the zone of Cosmoceras Parkinson at Halfway House,
Wyke Quarry, and Burton Bradstock.
The longitudinal lines well distinguish this species. It is also
ornamented with longitudinal furrows, which vary slightly in depth,
as also does the species in thickness.
QpPELIA SUBRADIATA (Sow.).
1825. Ammonites subradiatus, Sow. Min. Conch. pl. 421. fig. 2.
1845. A. subradiatus (Sow.)?, d’Orb. Terr. Juras. pl. 129. fig. 3.
1854. A. subradiatus (Sow.), Morris, Catalogue, p. 295.
1856. A. subradiatus (Sow.), Oppel, Juraformation, p. 372, fig. 26.
Localities. Zone of Cosmoceras Parkinsont at Broad Windsor,
Crewkerne Station, Bridport, &c.: rather common.
THE INFERIOR OOLITE OF DORSET. 607
Termination from the inner whorl nearly straight, then a rather
fine horn, then a curve back, and produced on the ventral area.
OppELia suscostata (J. Buckman).
1881. Ammonites subcostatus, J. Buckman, Quart. Journ. Geol.
Soc. vol. xxxyli. p. 63, no. 8.
1845. A. subradiatus, d’Orbigny (non Sowerby), Terr. Juras.
pl. 118. figs. 1, 2.
This species was figured by d’Orbigny as the large form of Oppelia
subradiata (Sow.); but I am convinced that it is distinct. It has a
far larger umbilicus, coarser ribs, hardly a distinct keel, and is far
thicker.
Localities. Zone of Stephan. Humphriesianum at Oborne &e.:
rather scarce.
HapiocERAs oonitHicum (d’Orb.).
1845. Ammonites oolithicus, d’Orb. Terr. Jurass. tab. 126.
figs. 1-4.
1854. A. oolithicus (d’Orb.), Morris, Catalogue, p. 294.
1856. A. oolithicus (d’Orb.), Oppel, Juraformation, p. 573, no. 32.
Localities. It occurs in the Humphriesianum zone at Oborne and
Milborne Wick. Our specimens have a slightly smaller umbilicus
than those figured by d’Orbigny, but are exactly similar in all other
respects.
AMMONITES cADOMENSIS, Defrance.
1845. Ammonites cadomensis (Defrance), dOrb. Terr. Jurass.
pl. 129. figs. 9-11.
T am not certain to what genus to attribute this species.
Localities. This species occurs in the zone of Stephan. Humphrie-
sianum at Oborne. It israre. A few specimens possess the peculiar
termination. I have one specimen with it from Wyke Quarry, and
others from Oborne.
It may be also interesting to add that we have found the following
species of Ancyloceras &c. in the Inferior Oolite :—
Ancyloceras annulatum, d’Orb. Terr. Jurass. pl. 225. figs. 1-7.
Humphriesianum zone at Oborne.
Anc. subannulatum, d Orb. Terr. Jurass. pl. 225. figs. 12-15.
Humphriesianum zone at Oborne.
Ane. bifurcatum, Quenstedt: syn. Hamites bifurcatus, Quenstedt,
Ceph. tab. 11. fig. 15.
Humphriesianum zone at Oborne.
Ane. bispinatum, VOrb.? Terr. Jurass. pl. 228. figs. 6-9.
It much resembles this species, but is from the top of the Hum-
phriesianum zone near Halfway House, and may be new.
608 ON AMMONITES FROM THE INFERIOR OOLITE OF DORSET.
Toxoceras Orbignyt (Baugier and Sauzé), d’Orb. Terr. Jurass.
pl. 232. figs. 1, 2.
From near Sherborne.
Since the above paper was written, we have made out the Yeovil
sands more clearly from some fresh sections. Just below the Mur-
chisone zone (the equivalent of the Gloucestershire Pea-grit) come
about 30 feet of sands. Then comes a marly bed about a foot thick,
containing Harpoceras opalinum, Lytoceras torulusum, Waldheimia
anglica, and Rhynchonella cynocephala. Below this come about
100 feet, sometimes more, of sands in which Lytoceras jurense (Zieten)
occurs along with Harpoceras Moore: (Lyc.) &e. These lower sands
therefore belong to the zone of ZL. jurense.
On the vexed question as to whether these latter belong to the
Lias or Oolite I have not formed an opinion.
Discusston.
The Prestpent bore testimony to the great industry and skill
shown by the young author in collecting from the richly fossiliferous
beds of the Inferior Oolite of Dorsetshire. He pointed out the
importance of having sections of perfect specimens of Ammonites
made, so as to show the relation of the body-chamber to the others
in these shells.
Mr. Huptestron referred to the difference between the views of
Mr. 8. Buckman and his father, Prof. Buckman, as to the value of
the zones of the Inferior Oolite and the geological age of the Yeovil
Sands.
Mr. CuarteswortH remarked on the absence of phragmocones of
Belemnites in Chalk rocks, and of the opercula of Ammonites from
many Jurassic rocks.
Prof. Srprey denied the universal absence of phragmocones of
Belemnites in the Chalk, and stated that it might be accounted for
by the condition of preservation of the fossils. In the same way the
absence of aptychi might be accounted for by the general explana-
tion of such facts given by Mr. Sorby, who showed that fossils
composed of the unstable substance aragonite were rarely preserved.
Prof. Brake thought that many of the so-called species of Ammo-
nites would prove to be only varieties of well-known ones. He
confirmed the views of the President as to the value of determining
the proportion of the body-whorl.
The PrestpEent stated that Mr. Buckman had adopted the views
of classification which he had himself long ago insisted on. He
accounted for the frequent absence of aptychi by the fact that the
body-chamber is not usually broken open. He also agreed with Mr.
Charlesworth as to the general but not universal absence of the
phragmocone in Belemnitella, and with Mr. Blake that many of
these Amamonite-forms could not be regarded as distinct species.
E. J. DUNN ON THE SOUTH-AFRICAN DIAMOND-FIELDS. 609
40. Nores on the Diamonv-FIELDs, Sour Arrica, 1880. By EH. J.
Duyn, Esq. (Communicated by Prof. Ramsay, F.R.S., F.G.8.)
(Read June 22, 1881.)
THE mining-operations carried on during the last few years at the
diamond-fields, South Africa, have brought to light some additional
- facts bearing on the formation of diamonds*; the most interesting
is the exposure, at all the old mines (Kimberley, De Beer’s, Du Toit’s
Pan, and Bultfontein), of considerable deposits of black carbonaceous
shale underlying the surface beds of grey shale.
By the removal of the diamond-bearing ground of the old vol-
canic “‘ pipes” constituting the above mines, the wall or rim is left
unsupported ; after rain immense masses of this shale, or ‘“ reef,”
as miners term it, fall into the excavated gulf, leaving excellent
clean sections of the horizontal strata; for the bedding of the shales
is horizontal, except where locally disturbed by intrusive rocks, or
at the sides of the “pipes,” where they are turned upwards for a
few feet, perhaps by the gabbro in the “ pipes.”
At Kimberley mine the surface-shales, grey or, in places, pink or
yellow, which contain remains of small Saurians, are from 40 to 50
feet thick; underneath are black carbonaceous shales, for the most
part arenaceous, and more than 100 feet thick. So combustible
are these shales that in a part of the mine where they were acciden-
tally fired they have smouldered on for more than eighteen months
and are still alight.
Time did not admit of a search for plant-remains; but a diligent
search, especially in the finer and more argillaceous beds, would
be almost certain of success. Thin seams of very impure coal full of
pyrites occur in the black shales ; and here and there a long flattened
piece of pure coal is found, probably the stem of some plant altered
to coal and flattened by compression.
At De Beer’s mine, on the north side, a somewhat different sec-
tion is laid bare. First there is, from the surface down, about 50 feet
of dolerite, then about 12 feet of yellow thinly laminated shales ;
beneath these are the black carbonaceous shales, corresponding with
those in Kimberley mine, and also containing thin seams, up to
1 inch in thickness, of impure coal.
The precise depth of these carbonaceous shales has yet to be
determined; but that they extend horizontally over the whole
country at no great depth below the surface there is no reason to
doubt; for wherever wells have been sunk in the neighbourhood of
Kimberley, De Beer's, Du Toit’s Pan, or Bultfontein, these black
shales have been encountered at depths varying from 40 to 60 feet
from the surface. These shales are to be traced cropping out on the
banks of the Modder river}, some forty miles from Kimberley, and
* [See E. J. Dunn’s previous papers, Quart. Journ. Geol. Soc. vol. xxx.
p. 54; and vol. xxxili. p. 879. ]
+ [Quart. Journ. Geol. Soe. vol. xxx. p. 582.]
Q.J.G.S. No. 148. 25s
610 E. J. DUNN ON THE SOUTH-AFRICAN DIAMOND-FIELDS.
again on the Riet river, still further away. How much further they
extend can only be determined by boring ; for the level nature of the
country prevents one from obtaining any knowledge of the beds
100 feet below the general level.
That the old mines are volcanic “ pipes,” and that they have
burst through these carbonaceous shales is evident. Is it not reason-
able to infer that the carbon, indispensable in one form or another to
the formation of diamond, was supplied by these shales ?
It is well known that at and near the surface, or while the work- ~
ings in the “pipes” were bounded by grey shale, the mines were
not so productive as at lower depths ; when the zone of black shales
was reached the diamonds were more plentiful and also of better
quality.
At Kimberley the improved yield as depth was attained was well
recognized ; and at Bultfontein mine so notably is this the case that,
though the surface-ground scarcely paid for working, the yield at a
depth of from 60 to 80 feet is most satisfactory. Jagersfontein, in
the Free State, again, is an instance of a mine poor at the surface,
but very profitable to work lower down.
So far as experience can be drawn on as a guide, it appears that
the yields of diamonds in these “pipes” are greatest when mining
is carried on in the portions of the “pipes” surrounded by carbo-
naceous shales, rendering it probable that these shales suppled the
element necessary to the formation of diamond.
A practical question of serious importance as regards the diamond-
mining industry here suggests itself: if the black shales supplied
the carbon of which the diamonds are formed, it is to be expected
that some diamonds would be found higher in the “ pipes” than
the black shale ; for the tendency of the molten rock would be to
rise, and this would also be the case with carbon in the state of
vapour; but is it probable that diamonds will be met with below
these shales ?
Already in three separate localities shafts sunk at the edge of
Kimberley mine have, at a depth of 300 feet, struck remarkable
intrusive rocks—amygdaloids, breccias, &c. that differ essentially
from any thing found penetrating the surface-shales. Whether these
are older intrusive rocks on which the shales were laid down, or
whether they are later than the shales and penetrate them is not yet
decided. ;
That the “pipes” will continue down for a vast depth there can
be no doubt; but if beneath the black shales the “pipes” have
traversed rocks devoid of carbon, are diamonds still to be expected
in them ?
Koffyfontein mine, on the road between Kimberley and Jagers-
fontein mines, has so far not proved rich at the surface. Many other
undoubted “pipes” have been opened and prospected near Kimber-
ley ; but subsequently they have been abandoned as unremunerative,
although some diamonds were obtained. It is very probable that
by deeper sinking in these localities richer yields would be found,
as the black shales are almost certainly below.
E. J. DUNN ON THE SOUTH-AFRICAN DIAMOND-FIELDS. 611
Should it prove to be the case that these carbonaceous shales pro-
vided the carbon for the diamonds, the conclusion is forced on us
that the original source of the diamond is the atmosphere ; for the
plants absorbed carbonic acid gas from the air, and in course of
time were entombed, and thus provided a store of carbonaceous
matter in the shales. Later on these shales were shattered and
engulfed in the molten rock. The carbon was then liberated in the
state of vapour by the intense heat; but, being under great pressure
in the ‘ pipes,” instead of escaping, it crystallized out as sparkling
diamonds.
The disclosure of such extensive deposits of carbonaceous shale
has other bearings quite as important as on the formation of dia-
monds. Hitherto nosuch deposits were known to exist in the Karroo
beds or Dicynodon series of rocks that cover such an immense area
in Cape Colony and the Free State. Vast plains broken by hills,
either isolated in groups or in long ranges, characterize the country
occupied by these rocks; the river-beds are generally shallow; and
thus it happens that until the southern limit of the Karroo beds is
reached, which is 200 miles direct from Kimberley, no section, even
to a moderate depth below the general level is obtainable.
‘At their southern termination these horizontal beds abruptly
cease, exposing their edges through a thickness of more than 3000
feet, and form the Nieuwveldt, Camdeboo, and Winterberg ranges
of mountains.
No seam of coal has been found along these well-exposed edges,
although well searched for. Very insignificant thin seams of black
shale do exist, also occasional plant-remains in the form of Glosso-
pteris and Hqwisetum, but no such shales as at the diamond-fields.
The remarkably pure anthracite found vertically intersecting the
rocks (Karoo beds) at Butfel’s Kloof, Camdeboo* has been proved
by boring to be the result of distillation, perhaps ensuing from the
action of intrusive rocks on the vegetable remains included in the
shales. At the above locality a large dyke underlies the outcrop
of anthracite, though at the surface it is several hundred yards
distant.
The trough of the great basin occupied by the Karrooy beds lies
south of the Orange river, and about east and west. Is there not a
possibility that these carbonaceous shales cropping out near the
northern limit of the Karroo beds may develop into true coal-seams
further south, or nearer the centre of the basin? A couple of bore-
holes would settle the point; and the pressing need for fuel at the
diamond-fields will ensure the trial being made.
In previous notes some dyke-like masses at De Beer’s mine were
described as noticeable near the surface; now that the workings
have reached a depth of over 100 feet these dykes are less equivo-
eal, as the rock forming them appears in almost its original con-
dition, and not decomposed as at the surface; it is of dark bluish-
* [See E. J. Dunn’s Report to the Colonial Parliament, 1879.]
+ |This name, as used by Mr. Dunn, excludes the Uppermost Karroo or Storm-
berg beds. |
28 2
612 E. J. DUNN ON THE SOUTH-AFRICAN DIAMOND-FIELDS.
grey colour and somewhat erystalline texture. It appears to differ
from the general mass filling the “ pipe” only in being fine-grained
and less liable to decompose. These dykes arefrom 2 to 3 feet thick ;
they cut through the gabbro filling the ‘‘ pipe,” and the carbonaceous —
shales, grey shales, and dolerite that form the sides of the ‘‘ pipe.”
No similar dykes were observed in any of the other mines.
At Bultfontein mine the shales on the east side are much disturbed,
and are tilted in places at an angle of 60° away from the ‘“ pipe.”
There are numerous blocks and small pieces of dolerite in this
mine that have been so rounded by attrition against one another,
probably caused by the heaving of the mass when in a molten state,
that they resemble boulders and pebbles. These stones are not so
noticeablein any of the other mines as they are at Bultfontein.
As an instance of the value of the ground filling these “ pipes,”
the following (on good authority) is of interest :—
At Du Toit’s Pan 7000 loads, 16 cubic feet each, yielded, on an
average, diamonds to the value of £2 12s. per load.
Discussion
Prof. Ramsay said the facts mentioned were remarkable; and 1%
was extremely difficult to say what the circumstances were under
which diamonds were developed. |
Mr. J. Evans said that the author had in this paper gone further
than he had done in his previous communication. ese year small
diamonds had been shown at the Royal Society made, it was said,
artificially. It would be an experiment worth while for Mr. Hannay
to repeat, in the form of heating together pieces of carbonaceous
shale and of fusible igneous rock.
Prof. Srptry said the view of the author was a plausible one. He
himself had suggested that carbonic acid might have been carried
down by water, and then decomposed by the heat of the volcanos,
so that the carbon, when liberated, might become crystallized. The
general principle of the author’s theory might be true, though,
perhaps, not the precise application of it.
G. R. VINE ON STOMATOPORA AND ASCODICTYA. 613
41. Srvrran Untsrr1at Sromatoporz and Ascopicrya. By Grorcr
Rosert Vine, Esq. (Communicated by Professor P. Marri
Duncan, F.R.S., F.G.8.) (Read June 22, 1881.)
Tue genus Alecto was founded by Lamouroux in 1821 for a group
of adherent Polyzoa. In 1814 Leach had used the word Alecto for
a genus of Hchinoderms ; and Mr. Hincks says that it is still employed
in connexion with the Crinoidea. On this account its further use
for species of Polyzoa is objectionable. In 1825 Prof. Bronn used
the word Stomatopora, and in 1826 Goldfuss used Aulopora, as
names for individuals of the same genus as that founded by Lamou-
roux. For uniserial species d’Orbigny employed Prof. Bronn’s
name; but Blainville, Johnston, Milne-Edwards, Busk, and Defrance
used the original word “ Alecto” for species described by them in
their various writings.
The generic characters of Stomatopora have been given by various
authors ; and additions have been made from time to time. ‘The
rather full description given by Goldfuss* of Awlopora dichotoma,
together with figures of the species, renders identification compara-
tively easy. But somehow there has been a confusion in later
identifications, and the Awlopora intermedia t type of Minster has
been mixed up with Goldfuss’s type. Both of these are present in
the Jurassic formation; and it is, I will admit, rather a difficult
matter to say where the one ends and the other begins. If, how-
ever, authors would distinguish between the two types, we should
be able to get at the true range of the species, because each has an
individual facies of its own. Hall, in describing the species found
in the Trenton Limestone of Americat (Trenton Falls, Oneida
county), makes this distinction:—In <Alecto inflata we have the
tubes short and individually separate; whilst in Aulopera arachno-
adea the tubes are not distinct or separated from the general con-
sistence of the branch. Jules Haime, in his descriptions of the
fossil Bryozoa of the Jurassic rocks, places the whole of his species
under one genus; and I prefer this method rather than object to it.
Thus, Stomatopora antiqua from the Inferior Lias of Valicre, S.
Terqueni from the Inferior Oolite, and S. Bouchard: from the Ox-
ford Clay are of the Aulopora intermedia type; and this holds good
with species found in our own country. Stomatopora dichotoma,
S. dichotomoides, D’Orb., and S. Waltoni are of the same type as
that given by Goldfuss as Awlopora dichotoma. In S. Desondona,
Haime, from the Inferior Oolite of Longwy, we have a passage-
form between Aulopora intermedia and the genus Proboscina, and
then species of Proboscena passing by gradations, with a tendency
on the one hand to the [dmonew, and on the other to the larger
* Petrefacta Germania, p. 218, pl. 65. f. 2.
+ Ibid. p. 218, pl. 65. £1.
{ Palzontology of New York, vol. i. p. 77.
614 G. R. VINE ON SILURIAN UNISERIAL
Stomatopore. There are in all the species and genera named indi-
vidual characters, if isolated, that would indicate affinities in the
whole group; and Mr. Hincks is wise in grouping all these genera
under one family name, that of the Tubuliporide.
Prof. H. Alleyne Nicholson, in working out material snbmitted to
him for examination by Mr. U. P. James, of Cincinnati, and also
material collected by himself, saw fit to rename the species of
Hall Hippothoa inflata, and, according to his description, shifted
the species from the suborder Cyclostomata to that of the Cheilo-
stomata of Busk. I could not from the first agree with the Pro-
fessor; but I was unable to dispute the point raised by him other-
wise than by the mere expression of opinion ; for up to the present
time no record has been given of species of Stomatopora found in
our own Paleozoic rocks. I am now able to carry back the true
uniserial Stomatopore to the Lower Wenlock Shales of Shrop-
shire.
It may be as well to say a few words about the material used by
me for this and other papers (to follow) on Silurian Polyzoa. It is
now pretty generally known that, for the purpose of assisting Mr.
Thomas Davidson, F.R.S., in his labours on the Silurian Brachio-
poda, Mr. George Maw, F.L.S. and F.G.8., of Benthall Hall, Shrop-
shire*, has had washed and carefully picked, for Brachiopoda, about
18 tons of Wenlock shales. The débris of these washings were after
this laid aside for the use of other specialists. Some time since I
applied to Mr. Davidson, and afterwards to Mr. Maw (Mr. Davidson
supporting my request), for some of this refuse, for the purpose of
working out stratigraphically the Polyzoa and smaller Actinozoa.
My request being granted, Mr. Maw sent me on the 19th of March
over two hundredweight of the débris for this purpose. I intend
to use the whole of this material honestly ; for I feel convinced that
it can be only by labours such as these that a true idea of the
abundance of the Polyzoal life of former epochs can be obtained ;
and, though picking out fragments from such a mass, by the aid of
a hand-glass, may be both painful and tedious, I shall prefer to
work on different groups, as material accumulates, rather than delay
writing till the whole has been picked. I have already gone over
about thirty pounds of the débris from the eleven localities and ho-
rizons ; and it may be interesting, as showing the difference between
the shales of the Carboniferous and the shales of the Wenlock series,
when I say that a single pound of unwashed Hairmyres clay would
yield me in the washing more individual specimens than I have been
able to get from the thirty pounds of the Wenlock débris. In the
Carboniferous the fragmentary organisms are tolerably well pre-
served and perfect; in the other the Polyzoal remains seem to have
been much waterworn, but, with the exception of one locality, not
sufficiently injured to prevent identification. |
We are indebted to Prof. Hall for the first indication of the ex-
istence of uniserial Stomatopore in Silurian rocks. It is quite
* See Geological Magazine, Jan., March, &. 1881.
STOMATOPOR AND ASCODICTYA. 615
possible that Lonsdale and other workers on the Silurian organisms
may have had a previous knowledge of the fact of their existence in
these rocks; but no detailed account was furnished. For the work-
ing-out of these and other forms of Stomatopora we are equally in-
debted to Prof. Nicholson, M.D., F.G.S., &e.
Silurian Stomatopore.
1. SroMATOPORA INFLATA.
Alecto inflata, Hall, Paleont. of New York, vol. i. p. 77, pl. xxvi.
figs. 7a, 6, = Hippothoa inflata, Nicholson, Ann. & Mag. Nat. Hist.
Feb. 1875, pl. x1. figs. 1, la.
“ Zoarium* attached, arachnoid; zowcia short, much expanded
above, contracting at the aperture and narrowing rapidly below:
orifice large, opening obliquely upwards.”
This is Hall’s description of his species. Nicholson says that the
branches of his specimens are linear, and the “cells uniserial and
pyriform, each springing by a contracted base directly from the cell
below ; about four cells in the space of one line.” There is nothing,
however, in his description that would ally the species with the
Hippothoe ; but in working out my own Upper-Silurian types I have
given prominence to every feature that had any tendency to a Hippo-
thooid character.
The geological position of Hall’s species is the Trenton Limestone.
Nicholson’s specimens are from the Hudson-River Formation, Cin-
cinnati Group.
2. StoMaToPoRA DissIMiLis, mihi. Figs. 1-8 (p. 616).
Zoarium adnate, branching, generally attached to stems of Cri-
noidea, very rarely to broken shells; branches lmear, sometimes
wavy and anastomosing. Zoecia invariably uniserial, and, in the
best preserved, very finely ribbed transversely ; the oral extremity
slightly raised ; orifice circular or subcircular. Occial cells rather
ventricose and strongly ribbed (?). Each normal zocecium about
half a line; average about 6 to 34 lines.
Loe. Upper Silurian; “ Buildwass beds,” Harley, near Wenlock,
rather rare; also base of Wenlock shale, Buildwass Bridge, Shrop-
shire, rather common.
I have not found any specimens of this species in any other of
the eleven localities which I have searched for Polyzoa. In search-
ing the material from these two localities, I found it to my interest
to examine on both sides every fragment of shell and Crimoid that
came under my glass; the consequence of this is that I have speci-
mens, more or less perfect, of about fifty colonies. The drawings
are made from three of these, because they afforded me better facies
than the others. What I have given are characteristic of the
whole.
* To present a uniformity in the descriptions, I change the exact words of
authors to those in present use : thus, Hall's word “Coral” is changed to Zo-
arium, “ Polyzoary” of authors to the same.
G. R. VINE ON SILURIAN UNISERIAL
Figs. 1-8.—Stomatopora dissimilis, Vine, from the Buildwass beds,
Upper Stlurian, Shropshire.
| 7
jan
|
(cree /
Yp
I}
Ups
>"
AW
Te
a
Ce i
IN
1. Colony adherent to Crinoid stem. \ Hach of these colonies has been drawn
| with the Camera lucida, from three
5 es f separate specimens on Crinoid stems,
the habit of each colonial growth be ing
somewhat dissimilar in character.
2. 99 99
aed
%
99
STOMATOPORZ AND ASCODICTYA. 617
Fig. 4. Fig. 5.
4. Profile of two cells from No. 3 colony, only lower down on specimen.
5. Magnified cell on same colony (fig. 3, a).
6. Three cells from same colony (fig. 3, 0).
7. Cell from same colony, with caudate elongation (fig. 3, c).
8. Cell from another colony. The stoloniferous processes on specimen No. 3
do not belong to the Polyzoal colony, but to Ascodictyon. Upper Silurian,
Buildwass beds, base of Wenlock shale, Shropshire.
The habit of the colonial growth, as given in fig. 1, is similar
to that of Aulopora dichotoma, Goldf. Generally speaking, about
every second cell gives origin to a fresh one; and this is the be-
ginning of a new branch. I cannot, however, give this as a cha-
racter, on account of its variableness. The origin of fresh colonies
of this beautiful species is a most interesting study. Without
speaking positively on this point, I have in one small fragment
probable evidence that clusters of cells are developed from one of the
‘“‘ rosettes” otf Ascodictyon stellatwm, Nich. and Ether.* Around
this cluster primary cells of various colonies are disposed ; some
colonies have a linear arrangement of from three to five cells; the
primary cells are also disposed singly on different parts of the frag-
ment of broken shell; a larger mass of cells clustered in one spot
give origin to several linear branches of what I am disposed to
believe are new colonies. It may, however, be possible to explain
this feature by stating that one rosette gives origin to several linear
branches, and the whole clustered together would be the parental
nucleus of one colony variously disposed. There is sufficient evi-
dence to show that some colonies at least sprang from an inde-
pendent primary cell.
Amongst living Stomatopore a most remarkable feature is shown
in the figures of S. fasciculata, Hincks, pl. lix. figs. 4,57. In his
descriptive text (p. 441) Mr. Hincks separates this from all other
* Ann. & Mag. Nat. Hist. June 1877.
+ Hincks, Brit. Marine Polyzoa, vol. i1.; text, vol. i.
618 G. R. VINE ON SILURIAN UNISERIAL
known species, and places it in a division by itself (C. Colony
clustered). In the figure there are several peculiar clusters of cells,
including from two to five or seven cells. There are no stoloni-
ferous processes. In comparing the feature given here by Hincks
with that of Nicholson’s figure of Ascodictyon stellatum, and both of
these with my own specimen, I cannot arrive at any other con-
clusion than that some of the Ascodictya of the Paleozoic rocks
are in some way homologous with the cluster found upon Hincks’s
unique and solitary specimen of S. fasciculata.
The profile of two cells, fig. 4, shows the true Stomatoporous de-
velopment. There are some cells in fig. 3 that are of a most pecu-
liar character. They differ in a few particulars from other cells ;
and these I have ventured to suggest may be the ocecia of the
colonies. I may, or I may not, be right in my conjecture on this
point. Unless these be ocecia, I have not been able to trace in any
other cells the least indication of ovarian chambers. 5 is a good
illustrative example of the cell referred to. Other points of struc-
ture are alluded to in the description of the figures.
In the Annals and Magazine of Nat. History for June 1877, Messrs.
Nicholson and Etheridge, Jun., described and figured a most peculiar
and ‘‘anomalous genus of Paleozoic fossils.” The name given to
the group was Ascodictyon; and several species were described as
found in Devonian and Carboniferous rocks. The systematic po-
sition and affinities of the fossils were not established by the authors
when the paper was written. From material in my own cabinet I
ventured to suggest, in a letter to Prof. Nicholson, what, judging |
from the Carboniferous fossils, I believed to be the probable affini-
ties. JI have now discovered in the Silurian shales of Shropshire
several specimens of the species given by Nicholson; and so eare-
fully are the characters of the Devonian fossils made out, that I
can trace in the Silurian specimens a most remarkable resemblance.
In the stellate rosette and stoloniferous processes there are differ-
ences so slight that I was inclined to place my own fossils under the
same generic and specific names, distinguishing one only with a
varietal term *.
3. ASCODICTYON sTELLATUM, Nich. & Eth., Jun.
I have only two specimens of this type. There are a few differ-
ences, which it may be well to indicate by giving it the varietal
name, siluriense, mihi.
Colony composed of calcareous clusters of ovoid cells, having a
somewhat stellate character ; each cluster containing from four to
seven cells, which are connected together by creeping filamentous
cords, some of which anastomose at intervals.
Loc. Buildwass beds, near base of Wenlock Shale, Shropshire.
* Since this was written, I have been able to work out fuller details of this
most remarkable group ; and I may add that Professor Nicholson has furnished
me with specimens of his so-called Hippothoa inflata, particulars of which will
be given in a future paper on the Polyzoa of the Wenlock Shales.
STOMATOPORZH AND ASCODICTYA. 619
4, Ascopicryon RADIANS ?, Nich. & Ether. (Provisional placement.)
I have several colonies of this beautiful type apparently similar
to those found in the Carboniferous rocks of Scotland. The colonies
are not so prolific, however, in the Silurian as they are represented
to be in the Kast Kilbride district. In the Silurian the clusters
rarely exceed two or three ; in many cases there is only one stellate
group of “elongated vesicles.” For the present I merely record
their discovery, reserving more detailed description for some future
time when my material is better worked.
Loc. Buildwass beds, near base of Wenlock Shale, Shropshire.
Hab. On stems of Crinoidea and fragments of shell.
Without committing myself to any systematic classification (other
than that suggested in the text) of these peculiar fossils, I think it
would be unwise and ungenerous on my part to conclude this paper
without speaking most approvingly of the labours of Prof. Nicholson
and Mr. Robert Etheridge, Jun., in the same direction as my own.
Prof. Nicholson remarks, in the paper on Ascodictyon™, that this
“‘ genus, so far as our present knowledge goes, is confined to the
Devonian and Carboniferous periods.” I am now able to extend
its range.
Ascopictyon, Nich. & Ether. Jun.
Upper Silurian...... A. stellatum, var. siluriense, mihi, ............ Shropshire.
Middle Devonian... A. stel/atwm, Nich. & Eth. ..................... Hamilton, Ontario.
Fs cd PAL USUTOTIME, | ., Ss NS ee 7": 55
Upper Silurian...... A. radians?, ,, »» my own cabinet.. Shropshire.
Carb. Limestone ... A. radians, Ps 3 ‘ s Scotland.
33 32 A. stellatum 99 9? 29 De) 29
SroMaTopora, Bronn, uniserial species.
Lower Silurian...... IS) SIGE: ol 1 AR Ree oe Trenton Limestone,
America.
_ ay Oleoere S. inflata, (Hippothoa inflata, Nich.) ......... Hudson-River For-
mation.
Upper Silurian...... S. disstemilis, Vine; my own cabinet ......... Buildwass_ beds,
Shropshire.
12/:7170 1710 eee S. Voigtiana, King. Humbleton, York-
shire.
Discussion.
The Presrpent stated that very important results were being ob-
tained from these washings of Mr. Maw’s of Upper Silurian rock.
Some of those obtained by Mr. Davidson were of the highest value.
Aulopora had been made a receptacle for very various forms.
Prof. Duncan said that the value of Mr. Vine’s researches was.
very great. The numbers of Polyzoa produced were very great; and
some of the Heteropore were singularly recent in aspect.
* Ann. & Mag. Nat. Hist. June 1877.
620 PROF. H. G. SEELEY ON THE REPTILE
42. The Reprite Fauna of the Gosav FORMATION preserved in the
Gurotogican Musrum of the University of Vinnna. By Prof.
H. G. Susruy, F.R.S., F.G.S., &c., Professor of Geography in
King’s College, London. With a Nore on the Guotoetcan
Horrzon of the Fosstts at Nrvz WEtt, west of WrENER Nuvstapt,
by Enpw. Svzss, Ph.D., F.M.G.S., &c., Professor of Geology in
the University of Vienna, &c. (Read June 8, 1381.)
[Puates XXVII.—XXXT.]
ConrTENTS.
INTRODUCTION.
Historical review ; condition of specimens.
Dinosavrtia.
Dentary bone and teeth of Mochlodon Suessvi (Bunzel).
Skull of Struthiosaurus austriacus, Bunzel; with a note on the base of the
skull of Acanthopholis horridus, Huxley.
On the genus Cratzomus, an armoured type with powerful fore limbs.
Mandibles and teeth, probably referable to Cratgomus.
Crateomus Pawlowiischti, Seeley, vertebral column, ribs, dermal armour,
scapula, humerus, femur, tibia.
Crateomus lepidophorus, Seeley, coracoid, scapula, humerus, femur, tibia,
fibula, metatarsal bone, claw-phalange, dorsal vertebra.
Tooth of Megalosaurus pannoniensis, Seeley.
Femur of Ornithomerus gracilis, Seeley.
Lower jaw and maxillary bone of Doratodon carcharidens (Binzel).
Femur and humerus of Rhadinosaurus alcimus, Seeley.
Scapula, humerus, and femur of Oligosaurus adelus, Seeley.
Humerus, scapula, vertebrae, and armour of Hoplosaurus ischyrus (Seeley).
CrocopiLia.
Vertebral column, femur, fibula, ulna, radius, &c. of Crocodilus proavus.
CHELONIA.
Costal plates, postfrontal bones, and scapula of Plewropeltus Suessii, Seeley.
Costal plates and plastron of Hmys Neumayri, Seeley.
LAcervinia.
Vertebra of Argosaurus gracilis, Seeley.
ORNITHOSAURIA.
Ornithocheirus Binzeli, Seeley.
INTRODUCTION.
Historical Review.
Tur Gosau formation, nearly corresponding in age to the Upper Green-
sand of this country, is represented at Neue Welt, near Wiener Neu-
stadt, by freshwater deposits full of such freshwater shells as Melania
and Unio, and land-plants such as Banksia and Pecopteris. The for-
mation and its fauna have been described by Profs. Suess, Zittel, and
many others ; but, although the late Dr. Stoliczka detected a tooth
imbedded in the coal of the formation, no important knowledge was
obtained of the vertebrate fauna of the Gosau beds until Prof. Suess
—o a
REMAINE
C Berjeau lith | GOSAU REPTILIAN
,
)
4
a
f
} i
| ’
;
C.Berjeau tith
REPTILIAN RE
FAUNA OF THE GOSAU FORMATION, 621
was so fortunate as to obtain the assistance of Bergverwalter Paw-
lowitsch in conducting excavations. These were carried on with
admirable skill; timber drift-ways were driven into the rocks, with
the result that they penetrated into a perfect cemetery of the remains
of Cretaceous reptiles. The remarkable collection thus obtained
was intrusted for description to Dr. Emanuel Bunzel, whose memoir
upon it was published in 1871 in the ‘ Transactions of the Imperial-
Royal Geological Institution.’ Subsequently more specimens were
discovered ; and in Easter 1879 my honoured friend, Prof. Suess,
invited me to visit Vienna to examine these specimens, with the
object of making them available for the advancement of knowledge
by publication. With the assistance of the Royal Society I gladly
undertook this work, and spent a month in Vienna studying the
thousands of fragments which had been obtained. The great mass
of these, mere comminuted bones, proved of but little value; or,
rather, the time that I could give to their study enabled me to piece
together but few specimens that were likely to prove interesting.
There were, however, other important remains, which Prof. Suess
had already reconstructed and pieced together with great patience
and perseverance, that had produced many indications of lost animal
forms out of a chaos of débris. I soon found that Biinzel’s
views and my own presented certain differences. His memoir,
which extends to eighteen quarto pages, and is illustrated by eight
plates, describes the following species—Crocodilus carcharidens,
Iguanodon Suess, Struthiosaurus austriacus, and Danubiosaurus
anceps. Other remains are referred to the genera Hylcosaurus,
Scelidosaurus, and Lacerta; while certain specimens are classed as
‘“‘Crocodili ambigui,” Chelonians, and indeterminate remains. All the
specimens which he described are figured; but the artist has so im-
perfectly appreciated the details of character of the fossils represented
in Bunzel’s plates, that it is impossible to form from them a just
opinion of these fossil reptiles. After examining the specimens, I have
come to the conclusion that some of Bunzel’s identifications may be
modified. Jam unable to recognize Scelidosawrus, of which Bunzel
figures a claw-phalange, tail-vertebre, and dermal armour. Hyl«o-
saurus is another genus doubtfully cited, resting upon a single scute,
which it may be well to discard. Lacerta is a genus that certainly
_ cannot be recognized, although the author refers to it parietal and
postfrontal bones, the articular element of the lower jaw, and the
right side of the lower jaw, vertebra, fragments of ribs, humerus,
radius, and femora. But the genus Lacerta could here only be used
in the sense of animals of the Lizard group.
For reasons that will be adduced, the Crocodilus carcharidens,
founded upon a fragment of the lower jaw, cannot be referred to the
genus Crocodilus; while the Danubiosaurus anceps was founded in
error, and the remains, instead of being lacertilian, belong to other
orders and other parts of the skeleton than those identified. Stru-
thiosawrus being founded on a single specimen, remains an interesting
type; but I feel constrained to refer the Iquanodon Suessir to a
distinct genus.
622 PROF. H. G. SEELEY ON THE REPTILE
The vertebre, plate i. figs. 24-26, regarded as crocodilian, per-
tain to a small Dinosaur ; figure 27 in the same plate, regarded as
the dorsal rib of a Crocodile, I interpret as the cervical rib of a
Dinosaur. The vertebra, regarded as crocodilian, which are figured
in pl. 11. give evidence of a second and larger species of Dinosaur,
and exemplify its cervical, caudal, and dorsal vertebre.
On plate in. fig. 1, the specimen regarded as the right side of a
hinder dorsal rib of a Teleosaur I regard as the shaft of the femur
ot a new Dinosaurian genus. Figures 2—4, described as a crocodilian
femur, is the femur of the larger Dinosaur. Figures 5, 6, called
fragment of lower jaw of a Lizard, is certainly neither a fragment
of jaw nor a Lizard-bone, but the proximal end of a large rib of a
Dinosaur. Figures 12, 13, called the upper half of a crocodilian
humerus, I regard as the proximal part of a Dinosaurian fibula.
In plate iv. figs. 1, 2, classed as dermal bones of a Crocodile, I refer
to one of the large new Dinosaurs. Figure 3, described as the right
ium of Jguanodon Mantelli, is certainly a coracoid of a large Dino-
saur. The tail-vertebre on the same plate, referred to Scelidosaurus,
are caudals of the same Dinosaurian genus already referred to. The
figures 11, 12, called phalange of crocodilian, is a Dinosaurian meta-
carpal or metatarsal; and the claw-phalange (figs. 4, 5), referred to
Scclidosaurus, probably belongs to the same animal.
The figures of the remarkable skull of Struthiosaurus, represented
on plate v., are all unsatisfactory, since they give but a vague idea
of its structure. Figures 7-9, described as the rib of a lacertilian
(Danubiosaurus anceps), represent the scapula of the larger Dinosaur.
Figure 10, termed claw-phalange of Danubiosawrus, was shown by
Prof. Suess to be a piece of Dinosaurian armour, since he fitted it to
a remarkable horn-like scute of the larger new Dinosaur.
On plate vi. figs. 1-3, 1s represented another example of the large
Dinosaurian scapula, there interpreted as the rib of Danubiosaurus
anceps. Figures 4,5 are said to represent the left ilium of this
imaginary animal; but they are really the costal plate and blended
rib of a large and remarkable new Chelonian type. Figures 8-10,
termed bodies of vertebree of Lizard, are vertebree of the same species
of Crocodile represented on plate i. Figures 6, 7, described as the
articular part of the lower jaw of a Lizard, are really the articular
end of the lower jaw of a Pterodactyle of the genus Orithocheirus.
JT concur with the identification of fig. 11, as vertebra of a Lizard. The
bone represented in figures 12, 13, termed dorsal rib of Lizard, is the
fibula of a Crocodile. JI am unable to recognize satisfactory Lizard-
characters either in the humerus figured in this plate or in any of the
bones represented in plate vi., while that represented in figs. 22 and
23, termed a rib, seems to me to be a femur of a new Dinosaurian
genus. The Dinosaurian dermal armour in this plate, referred to
Scelidosaurus, must be associated with the bones of one or the other
of the large Dinosaurs already referred to.
All the specimens on plate viii. are Dinosaurian ; and I should only
differ from Dr. Buinzel in referring them, together with fig. 1 (which
he terms tail-vertebre of a crocodilian) to the principal Dinosaur.
FAUNA OF THE GOSAU FORMATION. 623
Figures 2-4 are termed by the author vertebra of a foetal Dinosaur ;
but I am not aware of any evidence which enables us to determine
a matter of that kind, and I refer it to the same animal as the so-
called Lizard-bones (pl. vi. figs. 14, 15, pl. vii. figs. 1-4).
Indicating these and some other differences of opinion from Prof.
Suess, and arranging the material, old and new, into species accord-
ing to my interpretation, | was invited to deal with the remains in
such a manner as my conclusions made necessary. As the time
available did not suffice for description of the whole collection, I was
generously permitted to borrow, from the museum of the University
of Vienna, the more important specimens, which required further
study or to be figured. The results I now offer to the Geological
Society. The subject confessedly presents great difficulties ; and in
the following memoir I have dealt with it to the best of my ability.
As already stated, the bulk of Dinosaurian vertebre, scutes, and
limb-bones are referable to two species of the same genus differing
in size and other characters. This genus is certainly new. But when
we come to examine the corresponding skull-fragments, there are two
species indicated (by lower jaws) which are both of about the same size.
There is also the somewhat smaller Dinosaur indicated by Biinzel
as Iguanodon Suess; and there are teeth that appear to be referable
to two other Dinosaurs, one resembling Lelaps or Megalosaurus, and
the other somewhat approaching the Scelidosaurian pattern. Hence
there is great difficulty in referring the right jaws to the skeletons ;
and there is absolutely no evidence to show whether the hinder skull-
fragment, called Struthiosaurus austriacus, belonged to one of these
species, or is the only specimen of the animal hitherto discovered. I
have therefore some doubt whether, in the endeavour to make the
subject clear, a synonym or two may not be introduced, which can
only be got rid of by the discovery of additional materials ; and I put
my views forward with some diffidence.
Of the new Chelonian indicated by costal plates which were sepa-~
rate from each other at the lateral margins, I find no other evidence
except postfrontal bones indicating a skull covered with an elaborate
pattern of minute scutes, and a strong but imperfect coracoid bone.
Both these latter remains, however, are so typically Chelonian,
although the skull-bones joined by squamose overlap instead of by
suture, that I have no doubt of the propriety of including the costal
plates in the Chelonian order, singular as is their form. This remark-
able animal is associated with Emydian types which differ in no
important respect from existing genera. The Pterodactyles are very
impertectly represented, and badly preserved, and require but brief
notice. The Crocodilians, however, are more curious, partly from their
remarkable resemblances to types previously known in the Green-
sand of New Jersey and Cambridge, and partly from displaying new
characters in the vertebre.
All the species hitherto discovered are peculiar to the deposit, and,
with the exception of those temporally referred to Crocodilus, Emys,
Ornithocheirus, and Megalosaurus, must, as it seems to me, be located
in new genera. The most important new type is the Dinosaur Cra-
624 PROF. H. G. SEELEY ON THE REPTILE
twomus, represented by two species; the other Dinosaurian genera
are Doratodon, Rhadinosaurus, Mochlodon, Ornithomerus, Oligosaurus,
and Hoplosaurus.
Condition of the Specimens.
Almost all the bones are in fragmentary condition, and somewhat
distorted by the effects of pressure. Being hollow, they have some-
times become greatly crushed ; and were it not that both right and
left bones are usually preserved, it would often be difficult to avoid
being misled by appearances which result from conditions of fossili-
zation. Unfortunately almost all the long bones have lost their
articular extremities, and although in some instances this may
perhaps be the result of fracture, yet in most cases it is certainly a
consequence of decay of the bones before they were covered up in the
deposit. I do not speculate as to whether the articular ends may
have been eaten off by large carnivorous contemporaries ; for there
are no indications of tooth-marks or other evidences of animals
which might thus have mutilated the specimens. No doubt to some
this condition would be proof that the remains were derived from
an older deposit; but since the Wealden and Cambridge Greensand
and Stonesfield Slate all have a number of bones in a not dissimilar
condition, it seems to me less hypothetical to find an explanation
of their condition in prolonged maceration, coupled with the litho-
logical and petrological modifications which the deposit has since
undergone. ‘There is, however, no record of natural association of
any of the remains; yet, as they have mostly come from the same
locality, it is probable that remains which agree in size and anato-
mical characters may, in most cases, with certainty be referred to
the skeleton of the same individual, since duplicate parts of the
skeleton are almost unknown in each species. There may perhaps
be a certain amount of doubt as to the correct association of the
remains which I have ventured to put together; but this is a doubt
which the anatomist will best appreciate who can realize the nature
of the studies which have led me to group the bones as here set
forth.
Mocutopon Svurssi (Binzel). (Pl. XX VII. fig. 1.)
See Biinzel, J. c. p. 8, pl. ii. figs. 7-11.
One of the most beautifully preserved specimens is a right dentary
bone of a small Dinosaur which at first sight exactly reproduces in
miniature the characters of the Jguanodon of the Weald; but it
differs in a character so remarkable that, had it occurred in a living
animal, no hesitation would have been felt in relegating the jaw to
a distinct genus. Anterior to the teeth, the symphysial extremity
of every /guanodon-jaw bends round so that the rami form a U-
shaped curve ; but this specimen is straight, and the anterior inward
inflexion is scarcely appreciable, so that the snout was evidently
sharply pointed, and therefore indicative of a new form of head.
The fragment is little more than 73 centimetres long, and the tooth-
bearing part of the jaw 17 or 18 millimetres; the height at the
hart. Journ Geol.Soc Vol. XXXVILPI. XXX.
a
Ws)
ie
quart Journ Geo
ore
Hanhart imp
PYILIAN REMAINS
aay ere See leriae
tan
Pt imp
a
anh
or
ast
iL
Quart Journ Geol. Sc
© Berjeau ith
GOSAU REPTILIAN REMAINS
FAUNA OF THE GOSAU FORMATION. 625
posterior end to the top of the coronoid process, which is imperfectly
preserved, is 34 centim. The external surface is smooth, rounded
at the base, with a strong rounded ridge descending from the ante-
rior margin of the coronoid process, and extending downward and
forward along the jaw, dying away in front, and placed well above
the middle of the side. Above this ridge the area of the jaw, ex-
tending inward to the alveoli, is flattened almost horizontally at
the back; but the area becomes more oblique anteriorly, and undi-
stinguishable as the ridge subsides. Along its upper and outer
margin towards this ridge is a series of foramina which are elongated
or ovate—four of them larger, and half-a-dozen smaller. The area
below the ridge is flattened towards the posterior limit of the dentary
bone; anteriorly it is flattened and pointed, being bevelled on the
inferior border for its union with the other ramus, and on the supe-
rior border terminating in an oblique area, which is compressed from
side to side and channelled by a somewhat deep groove. Whether
this groove is merely vascular, or whether it may have contained a
few premaxillary teeth, is a matter upon which I have no evidence.
It is about 16 millim. long, wider and deeper behind than in front,
and, as in the Wealden Jguanodon, has the inner border more ele-
vated than the outer border. Below it are three or four vascular
foramina. Both the inner and outer extremities of the jaw below
are roughened, and indicate that the symphysis was loose, but held
together by ligamentous union. As usual, the external outline of
the bone, when viewed from above, is moderately convex, and its
thickness from within outward continues to increase from before
backward almost to the coronoid process. The inner side, which is .
slightly crushed, displays ten alveoli. Portions of five or more teeth
are seen in the jaw; and there are impressions of others and empty
sockets, indicating ten in all. The first tooth, which is unfortu-
nately imperfect (wanting the extremity of the crown), is remarkable
for the smoothness of its inner surface, which, however, is elevated
into a very strong median ridge, leaving the sides slightly concave.
The serrations visible on the anterior margin are slight, and do not
extend down the tooth. It is not sufficiently elevated to have come
into wear. All the succeeding sockets are empty, owing to the teeth
having dropped out; but most of them show successional teeth
coming up, which have not yet reached the level of the outer alveolar
margin. ‘The second and third teeth are broken away on their ex-
ternal part, and not recognizable. The fourth tooth, also wanting
the extremity of the crown, still shows the same enormously deve-
loped median ridge; but external to it are, on each side, about half-
a-dozen fine parallel ridges which have sulcations behind them of.
about their own width. The fifth tooth only just shows the top of
its crown coming up low down in the alveolus. The sixth toothgis
’ the best developed, was apparently the largest, and occurs near the
thickest part of thejaw. Its pattern is like that of the last described ;
only the strong median ridge or keel is much sharper, and the lateral
concayities deeper, in accordance with the width of the tooth. The
lateral ridges run up and terminate in the sharp rounded lanceolate
Q.J.G.8. No. 148. 20
626 PROF. H. G. SEELEY ON THE REPTILE
margin, and give it a crenulate appearance, which is due to their
elevation. The median ridge terminates in a point, which is rounded
and does not project beyond the tooth-margin. The tooth is slightly
displaced, and leans backward towards the seventh socket. Low
down in the seventh socket the crown of another tooth is seen. The
eighth socket is empty. The ninth socket has lost the successional
tooth, but displays the external impression, and shows it to have
been marked with a median ridge and lateral finer ridges somewhat
radiating upward. The tenth socket appears to have been small; it
is imperfectly preserved, and there is no evidence as to its form or
character; but a groove, which is smooth, is placed behind the last
socket mentioned, and just in advance of the coronoid process.
Hence these teeth appear to differ from those of Jguanodon in the
persistent development of a powerful median ridge and in the stri-
ation of the external surface. Behind the alveolar border the bone
becomes squamous and thin, having overlapped the surangular bone,
though there is no trace of a separate coronoid element, from the
suture entering into the coronoid process. An opercular bone, or
its representative ossification, appears to have extended along the
broad subdentary groove at the base of the bone margining its upper
part, while the angular bone, if it were distinct from the surangular,
would appear to have reached far forward along the base of this
groove, and to have rested on a thin ledge of the dentary. The
submaxillary groove, in its anterior third, becomes shallow, but
persists to the symphysis. ‘The region of the symphysis has no defi-
nite outline.
Two separate teeth, both such as may belong to this species, have
been found. They are of small size, and may have belonged to
this individual specimen. One belongs to the lower jaw, and might
be the eighth tooth of the specimen described. The other is an upper-
jaw tooth. The tooth from the lower jaw (Pl. XX VII. fig. 2) shows
that the crown curves outward at a considerable angle to the fang; its
outer margin is worn, showing that the teeth worked together with
a scissors-like action, the lower-jaw teeth being, as usual, internal
to those of the upper jaw. ‘The external surface is marked with
about half-a-dozen primary ridges; between these, in the middle of
the tooth, are finer ridges; and across them run transverse lines of
growth. There is no median external ridge. The internal aspect
of the crown is essentially the same as in the specimens described
in the jaw itself. The median ridge, however, is not prolonged
down the fang; and hence there is a slight constriction at the base
of this ridge; and the elevated lateral ridges sharply define this
side of the crown from the smooth lateral areas. _
The upper-jaw tooth (Pl. XX VII. figs. 3, 4) has the crown simi-
larly curving inward from the fang. The fang is compressed from
side to side, so as to give a subquadrate section. There is a slight
constriction between the crown and the fang on the outer or cutting
edge, but no constriction on the inner edge. ‘The fang is imperfect
at the base; but the total length of fang and crown, as preserved, is
18 millim. The worn surface (fig. 4), like that aspect of the tooth
FAUNA OF THE GOSAU FORMATION. 627
itself, is convex from side to side. The unworn part of the crown
below is vertically striated; but the ribs are fainter than on the lower-
jaw tooth. The inner surface of the crown is subquadrate, marked
with eight vertical ridges, which are moderately elevated, stronger
and wider apart on one side of the tooth than on the other. The
height of the crown is about 8 millim., and its width about 7 millim.
Its thickness at the base is about 4 millim.
Parvetal bone of a small Dinosaur (probably Mochlodon).
(See Binzel, pl. v. fig. 11, p. 14.)
The parietal bone of a small Dinosaur (PI. XXX. fig. 1), which was
regarded by Bunzel as a Lizard, shows, as I take it, the parieto-frontal
suture in front, and an indication that the postfrontal bone was given
off from the expanded anterior outer corner, much as in Jyuanodon.
The under and interior surface of the bone, however, is much more
lizara-like in some respects, seeing that it did not enclose a brain-
case after the pattern demonstrated in Jguanodon, Hypsilophodon,
Struthiosaurus, and other genera. The bone was relatively thin, but
appears to have been united by a not very intimate suture to bone
below, which formed the lateral wall of the brain-case. The bone is
imperfect posteriorly, being fractured ; superiorly it is divided into
three areas :—a median triangular area with concave sides, which
becomes narrower posteriorly till it disappears at about the line of
fracture (this surface is slightly convex from side to side in front) ;
and two lateral areas for the attachment of muscles working the
lower jaw, which converge posteriorly, and in converging are more
highly inclined to each other. Their superior limit is sharply de-
fined by a ridge, which becomes elevated posteriorly, and is appa-
rently passing into a median crest, and is also elevated anteriorly at
the point where the postfrontal suture is visible. The length of
the fragment is 2 centim.; its width in front, as preserved, is 2
or 3 millim. more; its width posteriorly is 14 centim. There is
no foramen parietale. The characters are certainly such that the
bone might well be referable to the skull of a Lacertilian; but it
would be hazardous to determine absolutely on such evidence whether
the bone really pertained to Mochlodon Suessii, as is rendered pro-
bable by its Iguanodont form.
Scapula (probably of Mochlodon).
The imperfect proximal end of a small scapula (Pl. XXVIII. fig. 1)
presents somewhat Crocodilian characters. The fragment is only
4 centim. long. It shows the humeral articular surface and part of
the sutural surface for the coracoid. The character which especially
distinguishes it from Crocodiles is the extraordinary lateral position
of the humeral articulation, in consequence of the sutural surface for
the coracoid being prolonged beyond it. This articular surface is
24 centim. long, 15 centim. wide proximally, and narrower towards
the sutural surface. The bone is a little crushed, but was concave
from above downward, and flattened in the antero-posterior direc-
27 2
628 PROF, H. G. SEELEY ON THE REPTILE
tion. Hence the surface is narrower, more vertical, and more
elongated, and especially more.concave than in the Crocodile; but
there is a slight angle rising as a short ridge from the hinder exte-
rior corner of the articulation, directed upward and forward, repre-
sented in Crocodiles by a similar fainter ridge. Only the posterior
part of the coracoid suture is preserved. It makes an angle of 45°
with the humeral surface when seen from the front, and an angle of
90° when seen from the side. The bone is narrower in front and
behind than in the middle, where it is 12 millim. thick. So much as
is preserved is 24 centim. long. Its external margin is convex; the
internal margin appears to have been straighter. At the angle above
its union with the humeral surface there is a small depression.
Owing to the fact that the bone thickens externally with the humeral
surface, the area anterior to that surface is concave and smooth.
The concavity is directed obliquely downward and forward. There
are indications that the anterior margin of the bone was deve-
loped into an angular ridge, which may have corresponded with
that of the Crocodile. The visceral surface of the bone was concave
from above downward, and, though crushed, appears to have been
flatter from side to side, more rounded on the anterior margin, and
more compressed on the posterior margin about the humeral articu-
lation than in Crocodiles. The blade of the bone, however, was
similarly constricted at the fracture, where it is less than 2 centim.
wide and about 1 centim. thickras’ preserved, convex in front and
flattened behind. Though this bone is on the whole Crocodilian in
its characters, it is also Dinosaurian, and perhaps makes the nearest
approximation to the scapula figured by Prof. Marsh in the fore
limb of his five-toed Dinosaurian Camptonotus dispar.
SrRUTHIOSAURUS AUSTRIACUS, Biinzel.
(See Bunzel, pl. v. figs. 1-6, p. 11.)
The hinder part of the skull of a Dinosaur figured by Biinzel 1s some-
what difficult to describe, on account of the obliteration or obscurity of
the sutures ; and yet the anterior surface of the roof of the brain-case
is margined by a well-marked transverse suture limiting the front of
the parietal bone—a suture similar to that which persists in the skull
of the Fowl long after other sutures have become obliterated in the
hinder part of the cranium. The specimen certainly presents a remark-
able resemblance to the back of the skull of a:bird; but I believe that
Biinzel has attached more than due importance to this similitude,
owing to the circumstance that the true nature of the Dimosaurian
skull was even less perfectly known when he wrote than it is now.
He has supposed his specimen to be more complete than, in truth,
it is, being unaware, or unmindful, of the evidence that, external
to the parietal bone, the Dinosaurian skull has-an upper arch or
bar, like that so common in reptiles and unknown in birds, and
that, as a rule, there is also a lower malar arch, more or less deve-
loped, behind the orbit; and therefore it happens that the bone which
he regarded as tympanic or quadrate, and interpreted as Crocodilian,
is the paroccipital or opisthotic of modern anatomists, as, indeed,
FAUNA OF THE GOSAU FORMATION. 629
was long since appreciated by Mr. Hulke in describing his skull of
Iguanodon*, Therefore Bunzel’s Avian and Crocodilian affinities of
the skull both fall to the ground, owing to this fundamental miscon-
ception of its characters. Hence it appears to me desirable to describe
the specimen anew, in order to render its structure clearer. ‘The
specimen exhibits superior, lateral, inferior, posterior, anterior, and
cerebral aspects; and on each of these I propose to offer a few remarks.
The fossil, as preserved, is 63 millim. broad behind, and 5 centim.
high, owing to the downward direction of the occipital condyle ; for,
although the skull obviously increases in height as it passes forward,
the height from the base to the fronto-parietal suture is only 43
centim. The presphenoid bone is broken away; but the length
from the fracture or suture to the back of the occipital condyle is
43 centim., and to the back of the supraoccipital bone is 5? centim.
Superiorly and externally the cranial region is moderately convex
from side to side, and also exhibits a slight convexity from front to
back (PI. XX VII. fig. 6), especially towards the outer borders, indi-
eative, I think, of the parietal bone just reaching the margin of the
temporal fosse on the right side. The surface of the bone is rough,
with slight and irregular close-set elevations, not so distinct as
those of a Vrionyx, but certainly suggesting the surface that is
sometimes seen when the scutes are removed from a Chelonian
carapace. There is also a transverse furrow running across the
bone, rather behind its middle, nearly parallel to the convex posterior
border, and therefore curving backward. The width of this superior
surface, as preserved, is nearly 53 centim.; but then the bone is
broken on both sides, though it has become thin and separated late-
rally from the brain-case. Its antero-posterior extent in the middle
line where greatest is just over 3 centim. I have no doubt that
the transverse groove (Pl. XX VII. fig. 5) indicates the limit of the
parietal bone ; for the suture defining it is seen on the left side of the
cerebral surface and on the external lateral surface; but I cannot
trace it ucross the upper surface, and it may be that the suture is
obliterated by ossification, consequent upon a scutal covering. The
groove recalls those which occur on the skulls of Lizards such as
Trachydosaurus, while the texture of the bone is not dissimilar; and
hence it is also possible that we have here an explanation of the
absence of sutures, in the circumstance that they are covered up by
a layer of dermal ossifications. The parietal bone at the frontal
suture (Pl. XXVII. fig. 6) is 9 millim. thick; but at the transverse
groove the thickness is reduced to 7 millim., owing to cerebral exca-
vation beneath it. The area behind the groove terminates posteriorly
in a margin which is rounded, but suggests the idea that a plate
4 millim. thick in the middle, and becoming thinner laterally, was
superimposed upon the cranial bones. This region posterior to the
groove I suppose to be occupied by the supraoccipital bone.
The posterior aspect of the skull is chiefly remarkable for the
elevated border above the foramen magnum, which was evidently
* Hulke, Quart. Journ. Geol. Soc. vol. xxvii. p. 206.
630 PROF. H. G. SEELEY ON THE REPTILE
in somewhat close contact with the neural arch of the atlas, and for
the transverse grooves and muscular rugosities, which run between
this border and the slight groove defining the supposed cranial scute.
Hence the back of the skull is not vertical, like that of some Croco-
diles, and its superior margin is far from being as well rounded as in
very young Crocodiles ; and on the whole there is nothing to call for
remark as affihating this region to what is seen in either Crocodiles
or Lizards. The surface ascends somewhat obliquely, but im two
terraces ; that immediately above the ridge bordering the foramen
magnum is divided by it into two lateral portions. These lateral por-
tions are channels extending outward and downward, and widening
as they go. There are, on each side of the median vertical dividing
ridge in these channels, three large tubercles. Above the channels,
and as nearly as may be of corresponding size, is a pair of convex
surfaces, which are undistinguishable in the middle from the median
bar just referred to. They are margined above by the supposed
cranial scute, and, as they extend outward, widen and curve obliquely
upward; and a muscular ridge appears dividing the outer part of
this wedge longitudinally into two nearly equal parts. Hence the
pattern of the back of the skull as preserved is very like a capital
letter K placed transversely, so that the two diverging limbs corre-
spond to the ridges above the foramen magnum. The height from
the top of the foramen magnum to the summit of the back of the
skull is 2 centim. The transverse width over the supraneural ridges
is 4centim. The width of each ridge at its outer third, before its
upper border becomes concave, is 9 millim., the upper margin extend-
ing over the concave channel above it; higher up its width is little
more than half. The median connecting ridge between the two
transverse ridges at the back of the head is about 12 millim. wide.
Though the back of the head as a whole is convex from side to side,
it is concave from above downward in the median line. The foramen
magnum is slightly elliptical, being 17 millim. wide and about 15
millim. high. The skull presents the unusual condition that the
basioccipital condyle retreats below and in front of the upper border
of the foramen magnum, so that, placing the back of the skull verti-
cally, which puts the base of the skull horizontal, the back of the
brain-case projects for a centimetre behind the basioccipital condyle.
The areas at the outer and upper corners of the occipital condyle
are concavely notched, and at first convex from side to side, but
more flattened as they pass outward and upward. The depth from
the back of the skull to the base of the occipital condyle is 4 centim.
The base of the skull, as preserved, is triangular, 54 centim.
from the hinder border of the foramen magnum to the front of
the basisphenoid, or a fracture in front of the sella turcica. The
hinder border of the triangle is convex, and the lateral border is
concave, though all the borders are irregular. There is no sutural
distinction between the basioccipital and basisphenoid, any more
than between the basioccipital, exoccipitals, and supraoccipital bones.
The basioccipital condyle probably is formed to some extent by the
exoccipital bones, much as in the Crocodile, since foramina occur
FAUNA OF THE GOSAU FORMATION. 631
some little distance in advance of the basioccipital, which may be
presumed to penetrate the exoccipital bones and give passage to the
pneumogastric and hypoglossal nerves. The occipital condyle is
well rounded ; but its outline is subtrapezoidal ; its greatest width in
the upper third is 2 centim., its greatest depth 16 millim. The
under surface is deeply channelled, so that the thickness of the bone
behind the articular surface is one millim. ‘The region in front of
the occipital condyle is about 357 centim. long, fairly smooth, but
concayely excavated in the middle, both in length and breadth, rising,
however, to a rounded margin at the sides internal to the lateral
foramina. ‘The width across the pneumogastric foramina is 3 centim.
The lateral margin of the triangle is divided by a median convexity
into two concavities: the shorter, in front, is about 2 centim. long;
and the longer, behind, is a ttle more; while posterior to this, on the
left side, is a surface which appears to have been laterally sutural
and nearly vertical, while a suture on the opposite side shows that
the upper part of this mass consists of a small bone, which readily
comes away. Hence I interpret the lateral masses of bone external
to the foramen magnum as being the exoccipital bones, as in Croco-
diles, while the small bone above the outer border of the exoccipital
is the paroccipital of Owen; and I suppose the exoccipital to extend
forward so as to form the side of the wall of the brain-case; so that
no portion of the posterior lateral structure preserved can be the
quadrate bone, as supposed by Biinzel, and hence the analogy
attempted to be made out in this region of the skull with the
Crocodile can have no foundation.
I would next note the characters of the lateral aspect of the skull.
(Pl. XXVII. fig. 5). Here all the bones which are connected with
the roof of the brain-case are more or less broken, and the bones have
disappeared which formed the external suspensory arch for the lower
jaw, so that nothing remains but the internal part of the head,
which may be likened, perhaps, to that of a Crocodilian type in
which neither were the quadrate bones blended with its lateral walls
nor the pterygoid bones connected with its base. I fail altogether
to recognize a Lizard-like type, although, as at present used, the
term Lizard is almost large enough to include any thing. Forms
like Amphisbeena, which have the quadrate bone firmly wedged into
the skull and no trace of either of the postorbital arches, might well
be regarded as a distinct ordinal type; and there are some Dinosaurs
towards which the structures of the hinder part of such a brain-case
somewhat approximates ; but the cranial bones in ordinary Lizards,
like Iguana, form a part of the skull that is very imperfectly con-
nected with its roof, and very different from the structure seen in
Crocodiles and Dinosaurs, though other Lizards, ike Cnemidophorus
for instance, have a better union between the brain-case and the
surrounding bones; but I do not recall any type of Lizard that so
far corresponds in the characters of the bones covering the brain
with what is seen in Dinosaurs as to justify us in affirming that this
skull is lacertilian. Turning our attention first to the basal part of
the brain-case, it will be seen that the articular head of the basiocci-
632 PROF. H. G. SEELEY ON THE REPTILE ~
pital is directed almost vertically downward, showing, I think, that
the head must have been carried upon the neck as in Deer, Kangaroos,
and other animals in which the position of the neck is vertical. The
part of the basioccipital posterior to the sella turcica is flattened on
its cranial surface, gently concave from side to side, with a slight
median ridge. Then at a distance forward of about 3 centim. from
the occipital condyle, the brain-case thickens from below upward,
but does not present the cup-shaped depression seen in Crocodiles
and many birds, though its edge is obviously destroyed by fracture,
and must have extended some millimetres higher than the 13 milli-
metres preserved. At the border of this ridge, on each side, is a
large perforation for the second nerve. The inner and anterior wall
of the perforation is broken away ; and the transverse width between
the outer walls of these foramina is2 centim. Below these foramina,
and extending forward, are several others. First, on the right side
is a large foramen that runs obliquely outward and forward, pene-
trating into the brain-case. On the opposite side, instead of one
large foramen, there appear to be two, divided by a considerable
intervening piece of bone. I have no doubt that this foramen gives
passage to the fifth nerve. On the left side it is prolonged backward
and outward in a horizontal groove; and although there is a groove
on the right side, and though it is smaller and shallower, it does not
impress the margin of the bone. In advance of this foramen, and
below the sella turcica, in the anterior concavity of the bone, are
two other foramina, which appear to be vascular. The anterior one,
owing to fracture, is seen on the left side to curve obliquely down-
ward and forward, and open upon the base of the skull. Between
the outlets of these foramina, in the median line, is a portion of a
conical foramen, the anterior wall of which is removed by the
fracture.
The vertical fracture of the sphenoid (Pl. X XVII. fig. 6), where it
terminates, is triangular, 2 centim. wide, and about as high, the sides
being compressed so as to meet superiorly in a crest which rises in front
of the pituitary fosse, as in some birds, and not at all as in Crocodiles.
Its walls are concave at the sides; and posteriorly a slight longi-
tudinal ridge rises, which becomes directed at an angle inward and
upward to the ridge bordering the pituitary region behind. ‘The pit
for the pituitary body is about 12 millim. long and 9 millim. wide,
is concave from side to side, and margined by a sharp elevated ridge.
Its anterior part is overhung by the process of the sphenoid, which
rises above it. The posterior portion of the lateral aspect of the
skull consists of a small superior area, subtriangular, formed appa-
rently partly of the parietal and partly of the supraoccipital bones.
It is a smooth internal surface below the fractured roof of the brain-
case, directed obliquely outward, downward, and forward, and
traversed by a groove which probably indicates a suture between
the two bones. The posterior border is a sharp knife-edge, concave
from before backward. Under this edge a deep excavation extends,
penetrating to within half a centimetre of the brain-case. The ex-
cavation is smoothly concave, extends longitudinally, and is pro-
FAUNA OF THE GOSAU FORMATION. 633
longed backward and outward above the otic bones; but the sur-
face is prolonged obliquely outward and downward, so as to form a
smooth quadrate area, which rounds towards the base of the skull,
and terminates backward on the left side, where best preserved, in
a vertical lunate surface, convex behind and concave in front, formed
by the exoccipital and otic bones. In front these spaces slightly
converge, especially below and above; and behind the middle there
is a foramen a millimetre or two in diameter, apparently largest on
the left side, but smaller than might have been expected if it is the
entrance to the auditory chamber, which probably lies in the depres-
sion above it. From the lateral lunate surface to the inner wall of
the brain-case above the occipital condyle is 24 centim.
Finally there remains the interior cavity of the skull which held the
brain(Pl. XX VII. fig. 6). This does not present any great contraction
in the auditory region. Its extreme width behind is 17 millim., where
the auditory bones bulge inward after the manner of Crocodiles. The
transverse width of the brain-case is thus reduced to 13 millim. ; but
at the same time its height increases from 14 millim. behind to about
2+ centim. in the region of the auditory prominences, though the
extreme height of the brain-case is somewhat in advance of this
point, where it becomes 3 centim. ‘The width continues to increase
from behind forward to the parieto-frontal suture. It is greatest
in the upper third of the outline of the brain, where it amounts to
22 millim. A bone which in a bird might be regarded as the ali-
sphenoid, which lies above the sphenoid, appears to meet the parietal
and exoccipital by a well-defined suture, visible externally and in-
ternally, and running obliquely downward and backward. It is
difficult to speak with confidence of the limit of this bone on the
external surface, since as it extends backwards it is only preserved
on the left side. The suture from which it has come away is well
defined on the right side. Its anterior border is sharp; and the
external surface is concave from within and outward. This sharp
border appears to show that in this Dinosaur the brain-case was not
completely closed in front in the middle line. Anterior to the
highest point of the upper wall of the brain-case, which lies under
the transverse scute-like groove crossing the external surface, the
bone makes an angular bend forward; but though there are many
little irregularities of outline in the internal surface, there is nothing
so important as the bending inward and downward of the lower
part of the alisphenoids, which must have made the transverse
section of the cerebrum nearly circular at the parieto-frontal
sutures.
Imperfect as this description is, it will suffice to show that we
have here a Dinosaur of a type so different from that indicated by
the skull referred by Mr. Hulke to Jquanodon, as only to be classed
in a separate suborder; and if the base of a skull figured by myself
under the name Craterosaurus be, as 1 believe, also Dinosaurian,
that also indicates a subordinal type, and is totally distinct from
either of the others. These great differences of skull-structure lead
me to suspect that the Dinosauria are a far more important group
634 PROF. H. G. SEELEY ON THE REPTILE
than has hitherto been suspected *; and it may well be that different
genera present modifications which affiliate representatives of the
group towards Crocodiles on the one hand and birds on the other.
But I cannot believe that any order, however homogeneous, could
have spanned the interval between the Crocodile and the bird,
though there can be no doubt that this skull of Struthiosaurus makes
a nearer approach towards the bird than does the skull of any living
reptile ; its differences from the bird-skull are precisely those which
distinguish it from the Crocodile, little as we know or can infer con-
cerning the suspensory arches for the lowerjaw. In the base of the
skull not being covered with pterygoids there is a notable difference
from Crocodiles of the surviving type; but then the base of the skull
is not bird-like, any more than it is like that of any other animal.
It is one of the most distinctive points of the Dinosaurian skeleton.
Itwould bedesirable to compare this specimen with other Cretaceous
genera ; but, with the exception of Acanthopholis, none of these have,
as yet, ylelded any evidence of the brain-case. One fragment, found at
Folkestone at the base of the Chalk with the remains of the Acantho-
pholts horridus, is briefly referred to by Prof. Huxley; and on in-
spection it proves, though clearly allied, to belong to a different genus,
a fact that will be best demonstrated by a description of the specimen
and comparison of the figures (Pl. XXVIL. figs. 6 & 8 and 5 & 7).
Nore on THE Base oF THE SKULL oF Acanthopholis horridus, Huxley.
Professor Huxley’s account of the skull of Acanthopholis is so
brief that it would be difficult to be sure from it of the identity of
the specimen, especially since Prof. Huxley describes characters
which we are now unable to recognize, though it is, of course,
possible that the specimen is in a less perfect condition than when
originally noticed. I therefore reproduce Prof. Huxley’s original
remarks (Geol. Mag.1867, vol.iv., Huxley on Acanthophols horridus,
. 66).
ae Of the skull I possess only a very much mutilated fragment,
showing the basioccipital and basisphenoid. ‘The occipital condyle
measures 1-4 transversely, or has about the same diameter as that
of the skull of a Crocodilus biporcatus which measures 16 inches in
length from snout to occiput. But itis more elongated transversely
and excavated above than in the Crocodile, and the exoccipitals
enter more largely into its composition. The Crocodilian disposi-
tion of the Eustachian tubes is absent ; and the carotids run up the
side of the basisphenoid in Lacertilian fashion. The sella turcica has
a, well-developed posterior plate.”
This fragment (Pl. XX VII. figs.7 &8) comprises the base of the skull,
and includes the basioccipital and basisphenoid, which are completely
ankylosed, and give no indication whatever of suture. Iam similarly
unable to detect any sutural evidence of the exoccipital; nor can I re-
cognize the basioccipital condyle, which I believe to have been directed
* Professor Marsh, since this was written, has published a classification of
American Dinosaurs (Amer. Journ. Se. vol. xxi. p. 423).
FAUNA OF THE GOSAU FORMATION. 635
downward, and to have been largely removed by attrition, so that no
idea can now be formed of its relative depth. The presphenoidal part
of the specimen is broken away and terminates anteriorly in a trian-
eular transverse fracture (fig.8). The base of the skull, as preserved,
is 54 centim. long. In the middle it is 4 centim. wide, but narrows
posteriorly to the region of the condyle, where the bone is 33 millim.
wide. Auteriorly it also appears to contract a little; but at both
ends the external white film of bone has scaled off, leaving the dark
phosphatic substance below—a condition reminding one curiously
of the pale and dark mineralization of bones in the Cambridge Green-
sand. ‘This inferior region is concave in length, with a rounded
median ridge, and lateral concavities on each side of it in the middle.
Posterior to the middle area the bone is fractured inferiorly for a
length of 24 centim.; and this fracture I suppose to have removed
the lower half and characteristic form of the occipital condyle.
The basioccipital bone(P1. XX VII. fig. 7) terminates posteriorly in a
mass which, as preserved, is convex below and concave above, so as to
have a crescent outline, and is also moderately convex from side to side.
Above it is the brain-case, which certainly extended somewhat further
backward than the present limits of the occipital condyle, as is shown
by the form and character of the lateral walls. The superior surface,
however, of the occipital bone appears to curve convexly downward
as it extends backward ; and, as preserved, the bone is little over
1 centim. deep, and about 3 centim. wide at the origin of the con-
dyle, which is, as usual, defined by a lateral constriction that can
only be detected by careful examination, and is some distance pos-
terior to the lateral notches on each side of the base of the brain-
case.
The cranial cavity (fig. 8)is imperfectly defined, because there is no
portion of the roof of the brain-case preserved, and its lateral walls
are imperfect. It is evident, however, that it is higher than wide;
the posterior width in the region of the foramina for the hypoglossal
nerves is 28 millim., while the height appears to have been not less
than about 4 centim. On the right side a part of the inner wall of
the brain-case is exposed, showing that it is smooth, bulges inward
a little in the auditory region, and is inclined a little inward as it
extends upward. On the left side the bone is fractured, so as to
show that the hinder wall of the brain in the auditory region is 2
centim. thick, and extends outward transversely at a little higher
level than the base of the skull. It shows a horizontal semicircular
canal, which extends from the wall of the brain-case outward and
forward for a length of about 15 centim., as exposed, and is
about 3 centim. wide. The curve cannot be followed round; nor
can its relations to the other semicircular canals be definitely made
out.
Along each side of the floor of the brain-case, and under the
transverse jutting of its lateral walls, which extend out horizontally
behind, is a row of foramina which extends in a curve, just sepa-
rated from each other by bony interspaces. Six are visible on the
left side; on the right side there were certainly five, and may have
636 PROF. H. G. SEELEY ON THE REPTILE
been six (fig.’7). ‘These foramina are different from those of Struthio-
saurus or Iguanodon, and furnish a marked character, defining Acan-
thopholis. It may be difficult to correlate them with the foramina in
the back of the skull of a Crocodile; but since those perforations are,
for the most part, in the exoccipital bones, and extend downward at
the back of the skull, it is obvious that we have here in the longitu-
dinal arrangement something more nearly paralleled by Lizards,where
the twelfth, eleventh, tenth, eighth, fifth, and second nerves are given
off in more or less longitudinal series. The hindermost foramen
may be referred to the hypoglossal nerve, the next, perhaps, to the
pneumogastric nerve, then perhaps a vascular foramen. ‘The two
hinder foramina are much smaller than the third; and the third
foramen may probably be for the eighth nerve; the fourth is small;
the fifth is so large that it might well correspond to the fifth nerve.
The anterior direction of the sixth makes it probable that we have
here the foramen for the optic nerve; for though it is somewhat
smaller than might have been expected, it is given off from the most
anterior part of the side of the brain-case behind the sella turcica.
The anterior extremity of the basisphenoid is massive and wedge-
shaped, broken away on the compressed inferior lateral margins, as
well as in the front. A strong vertical plate rises in the middle, so
as to form the anterior border of the brain-case (fig. 8). The upper
margin is 34 centim. above the base of the skull, and it is nearly
2 centim. behind the anterior fragment of the basisphenoid preserved.
This plate therefore seems to me to be exactly in the position of the
posterior border of the sella turcica; but if so, the anterior border,
such asis seen in Struthiosaurus (figs. 6, 5), is entirely broken away.
What remains of the sella turcica is a concave base in front of the
plate, terminating anteriorly in two diverging concave streaks of
bone-surface, which probably represent the channels of the caro-
tids (fig.8). They extend downward and outward, making an angle
of 90° with each other, and do not appear to reach forward. On
each side of the posterior plate of the sella turcica there is a con-
cave notch in the skull-wall.
The skull diverges so far from both the Crocodilian and Lacertian
types that it may be as well to recognize it as equally distinct from
both. It resembles Struthiosaurus in the downward direction of
the occipital condyle, in the extension of the lateral wall of the
brain-case posterior to the condyle, in the transverse horizontal ex-
pansion of the exoccipital region in front of the occipital condyle,
in the massiveness of the bone in the auditory region, and in the
grouping of the foramina, so that the posterior three are inferior,
while the anterior three have a more anterior and lateral position ;
but the convex form of the base of the occipital bone, the immense
thickness of the basisphenoid bone, are matter for distinction, as is
the form of the alisphenoid in Acanthopholis. The resemblances,
however, are so remarkable as to show that these two genera are
near allies; and though we cannot infer with certainty the roof of
the brain-case of Acanthopholis from that of Struthiosaurus, or the
teeth of Struthiosaurus from those of Acanithopholis, yet they seem to
FAUNA OF THE GOSAU FORMATION. 637
me to show that Struthiosaurus was probably a Scelidosaurian, and to
open up a suggestive possibility of its claim to the jaws and teeth
which have a Scelidosaurian character. Future researches may
possibly demonstrate it to be the skull of Cratewomus; but as the
back of the skull of Siruthiosaurus is so different from that of Sceli-
dosaurus, I have not felt justified in adopting such a view.
CRATHOMUS.
The dermal armour of this genus presents a remarkable resem-
blance to that of the Scelidosaurian Dinosaurs. ‘The large supra-
vertebral scutes of the caudal region are compressed, and terminate
upward in a sharp knife-like edge. They are, perhaps, more like
the similar scutes of Scelidosaurus than those of Acanthopholis. The
flat dorsal scutes which were carried on the ribs were also keeled; but
the keel was relatively lower, and the plates were more or less ovate.
This, too, is a character paralleled in Scelidosaurus; but there are
also scutes without any ridge at all, and marked with deep vas-
cular grooves. These I regard as probably ventral. Coming probably
from the region of the shoulders are two remarkable scutes which
are quite unlike any thing at present figured. These plates, which
are excavated on the underside, terminated in a sharp spine at each
end; and the middle of the scute bore upon its surface a number of
conical ossifications, which have much the appearance of a group of
limpets packed close together. These ossifications have exactly the
appearance of the scutes of Hylwosaurus, so much so as to suggest a
doubt whether the armour hitherto referred to Hyleosaurus may
not be unankylosed scutes separated from the plate which carried
them, and really referable to Polacanthus, in which Mr. Hulke has
found an armour closely approximating to that seen in this genus.
Finally, there is a scute bearing a bone exactly like the horn-core
of an ox; this | am also disposed to refer to the fore quarters. The
distinctive features of this armour are the sharpness of the caudal
scutes and the form and patelloid incrusting of the cervical scutes ;
but in other characters it approximates to the genera already
named.
The vertebral column is remarkable for the forward extension of
the neural arch in the neck and the deep gap between the anterior
and posterior zygapophyses, the shortness of the neural spine, and
the biconcave form of the vertebrze, while the dorsal vertebree are
remarkable for the great strength of the ridge below the transverse
processes, the distinctness of the facets to which the ribs were arti-
culated, and the broad rounded base to the vertebre. The caudal
vertebre have somewhat the form characteristic of Acanthopholis,
having a groove in the middle line of the base ; but the single lateral
ridge is a point of distinction, though the renee bigs were ‘obviously
nearly allied to those of that genus. The ribs, in having the superior
margin flattened and widened to a greater extent than the depth of
the bone, present a character that is found in all reptiles which
carried heavy armour, but is especially characteristic of this form,
though, according to Mr. Hulke, met with also in Polacanthus. The
638 PROF. H. G. SEELEY ON THE REPTILE
fragments of jaw with the teeth, if rightly referred to this genus,
present a character similar to that of Priodontognathus, Scelidosaurus,
and Acanthopholis; but while nearly resembling Scelidosaurus, the
tooth-structure is distinctive in the character of the serrations, just
as the lower jaw is distinctive in its angularity and vascular foramina.
But it is the hmb-bones which best define Cratwomus. The scimitar-
shaped scapula, with its powerful acromion process, is altogether
distinctive, while what remains of the coracoid appears to indicate
an equally unusual form. The humeri are remarkably powerful, and
indicate an animal strong in its fore limbs, evidently a quadruped,
and therefore presumably carnivorous, since the herbivorous forms
have the fore hmbs feebly developed. The humerus, with a general
resemblance to that of Anoplosaurus, is far more robust, and indicates
a heavier animal: no bone anterior to the humerus is known. The
femur is distinguished from that of the Iguanodonts by wanting the
separate external trochanter at the proximal end. It has the arti-
cular ends powerfully developed, and, perhaps, most closely resembles
in general form that of Cryptosaurus eumerus of the Oxford clay. The
tibia is remarkable for the extremely compressed form and forward
development of the cnemial crest. The fibula, so far as preserved,
is very like the fibula of a bird, and bears a similar relation of size
to the tibia. The metatarsal and phalangial bones, if belonging to
this genus, rather indicate a flattened foot,terminating in claws which
were broad rather than sharp. Taken asa whole, far more difference
from Cratcwomus is found in described genera in the structure of the
internal skeleton than would have been inferred from either the
armour or the teeth; and it is quite possible that the armour, espe-
cially in Dinosaurs, may have undergone as little change as the
feathers of birds or scales of lizards, so as to be common to several
families.
Mandibles and Teeth probably referable to Crateeomus.
Three fragments of the anterior extremities of Dinosaurian lower
jaws have been found which indicate two species, though the re-
mains are so fragmentary that they cannot be defined with the
detailed accuracy which is desirable. Both specimens are of about
the same size, and belong to a genus which is closely related to
Priodontognathus. I will describe the more perfect specimen first.
This species is represented by a dentary bone (Pl. XX VII. figs. 9,
10), the anterior extremity of which is unfortunately not preserved ;
nor is the fragment complete on the hinder or lower border, though
it probably gives indications of the whole of the teeth. The alve-
olar border is bent in a sigmoid flexure (fig. 9); and the bone itself is
bent so as to present a flattened lower part at right angles to the upper
part of the side behind, but sloping more and more outward in front.
The lateral contour of the alveolar border is convex, rising higher in
the middle and descending to near the level of the base; it has
a width of about 6 centimetres. As usual with Dinosaurs, it is
higher on the external than on the internal margin. The teeth
were placed in sockets defined and separated by narrow bony inter-
FAUNA OF THE GOSAU FORMATION. 639
spaces. The sockets were circular, and indicate larger teeth in the
fore part of the jaw than in the hind part. ‘The alveoli for twenty
teeth are shown (fig. 9); they did not reach to the extremity of the
jaw; nor apparently was there any bony union between the rami; but
the small fragment anterior to the termination of the alveolar
margin is broken away. The length of the alveolar margin is
about 8 centimetres; and the extreme length of the fragment is
under 9 centimetres. The internal aspect of the jaw has at its
base a deep groove, which widens from before backward, and
passes close to the base of the jaw (fig. 9), though it appears
to slightly ascend, and no doubt lodged the opercular bone.
The basal margin below this groove is rounded; the surface above
the groove is smooth, and forms an obliquely twisted area, which
maintains a depth of about 13 centimetre, so far as it is preserved.
It is very slightly convex in length, but concave from above down-
wards, the concavity increasing forward owing to the increasing
twist in the bone. The depth of the jaw at the first alveolus is
18 millimetres. At the tenth alveolus it is nearly 2 centimetres ;
but the depth cannot be given further back, as the base of the jaw
is broken away. The hinder part of the inner alveolar border shows
indications of a squamous bone having come awey. This would pre-
sumably be part of the opercular bone.
The external surface (fig. 10), as already remarked, is traversed,
at least in part, by a strongly elevated ridge, which inclines a little
downwards as it extends forward, and dies away towards the anterior
end. The surface below this ridge is flattened, but very slightly
convex from above downwards, and, so far as preserved, is straight.
It shows a few deep narrow vascular grooves and markings for
vessels. The superior part of the side is obliquely twisted, be-
coming more and more horizontal behind, and more and more ver-
tical in front. In the middle of the side, both in length and depth,
are four large foramina (fig. 10), placed close together in a line,
seven millimetres below the alveolar border, and 7 millimetres above
the longitudinal angle in the middle of the bone. These foramina
and their interspaces extend over a length of about 28 millimetres.
The anterior one descends vertically ; the three posterior ones enter
the bone obliquely, being directed downwards, forwards, and inwards.
From the hinder and inferior corner of the last foramen a slight
ridge is prolonged backwards, which makes an angle in the upper
margin of the jaw. ‘The surface anterior to these foramina rounds
convexly from above downwards; and below the third to sixth
alveoli there are about four minute foramina, and below the seventh
and eighth, only much nearer to the alveolar margin, two others.
It would thus appear as though a series of foramina had extended
along the bone, of which the middle four had become greatly de-
veloped. ‘The thickness of the jaw from within outwards augments
along the line of the median lateral ridge; in front it is about six
millimetres, in the middle 12 or 13 millimetres, and obviously in-
creases aS it extends further backwards. What remains of the
inferior margin, the anterior 4 centimetres, is concave; and the
640 PROF. H. G. SEELEY ON THE REPTILE
margin curves downwards and inwards as 1 extends forward. The
fourth alveolus is the only one which displays an indication of tooth-
structure. It is the extremity of a compressed arrow-shaped suc-
cessional tooth with serrated border, more after the pattern of that
seen in Priodontognathus than in any other genus, but too imper-
fect to demonstrate the generic characters. It appears to be more
elongated than the teeth of any genus hitherto described. It may
pertain to one species of Cratwomus.
The other fragmentary pieces of lower jaws may or may not belong
to one individual. A terminal fragment pertains to the anterior end
of the right ramus. Two other and smaller fragments belong to the
left ramus; but they are so imperfectly preserved as to be scarcely
worth notice, although they are apparently quite distinct from the
species just described, if I may judge from the flatness of the in-
ferior surface of the jaw and the flatness of the lower part of the
side which was vertical.
The anterior extremity of the right ramus was loosely attached,
by a rough lunate surface about 17 millimetres deep and 8 milli-
metres wide, to the ramus on the opposite side. Its extremity is
bent a little inwards and downwards—the basal margin being con-
cave from in front backward, and the prolongation of the alveolar ~
margin convex. The fragment is 4 centimetres long; and though
upwards of 3 centimetres of the alveolar margin are preserved,
I do not recognize with certainty any tooth-sockets. If such
exist, they are three in number, and are indicated by small round
sockets placed just behind the symphysis; but as the whole anterior
end of the bone is covered with vascular foramina, and there are
corresponding foramina external to these possible sockets, it is not
improbable that they are foramina also, since they present no dis-
tinctive alveolar characteristics. The jaw thickens a little in
front here; it is bevelled, looks obliquely forward, upward, and,
perhaps, outward, and has the appearance of having utilized the
foramina in the nutrition of a pad. This surface is about 32 cen-
timetres long, and above the symphysis is 13 millimetres wide, but
becomes narrower posteriorly, where it terminates on the inner edge
of the jaw in a sharp margin, external to which two large oblique
foramina appear at intervals, the second of which seems to be ex-
ternal to the first tooth-socket, which is compressed from side to
side, if it really be a socket, of which there is some doubt. At this
point the depth of the jaw is about 23 centimetres. Below the an--
terior area described, the upper portion of the side which is smooth
begins to be concave from above downwards ; and the lower part of
the side which is rugose is here convex, though it may, perhaps, as
indicated by a fragment already referred to from the other side of
the jaw, become flattened in its posterior extension. The specimen
shows no trace of the groove on the inferior margin of the inner
side seen in the specimen already described; and the appearance of
a groove in the upper part probably results from fracture. The
internal surface is smooth and concave in length. The thickness of
the jaw at the posterior fracture is about 11 millimetres; the base,
FAUNA OF THE GOSAU FORMATION. 641
which is flattened, is nearly at right angles to the internal and ex-
ternal surfaces, and altogether unlike the narrow rounded base
which characterizes the species previously described. This, with
the less extension of the alveolar margin forward and greater
thickening of the extremity of the jaw to form the parrot-like ter-
minal surface, constitute specific distinctions.
Teeth.
The teeth have very much the aspect of having been eaten
(Pl. XXVIT. figs. 11-16), or at least exposed to some solvent which
may have slightly dissolved their surfaces; but the contours are
sharp and well preserved ; and though the fangs are in some cases
broken, the teeth do not exhibit the indications of ordinary wear.
It is very difficult, since they only number nine, to judge whether
the differences which are to be detected result from relative position
in the jaw, or whether one modification at least is not, as I am
inclined to believe, of specific importance.
These teeth have a triangular crown and a compressed fang.
There is a cingulum at the base on the outer side only; but it
merely serves to give a compressed aspect to the base of the
crown and to thicken the top of the fang. Even these teeth
exhibit certain modifications. First, there is one with the fang
perfect ; and this shows that it 1s closed ; and on the inner side at
the base it curves a little and shows an impressed area, as though
a successional germ had rested there; the fang in its upper part is
slightly concave from side to side. The tooth is bevelled off obliquely
on each side by the cutting-edge of the crown (Pl. XXVII. fig. 13).
The other side has a transverse cinguloid ridge, considerably lower
in position than the bevellings (fig. 14). It extends up towards
the bevelled corners at the sides. The crown is convex from side to
side; but the median longitudinal ridge is not distinctly defined.
Below the cinguloid ridge the tooth contracts from side to side.
The extreme length of the tooth is over 9 millimetres, the extreme
width of crown is about 53 millimetres, and its length down to the
base 5 millimetres. The width of the fang becomes reduced to
between 3 and 4 millimetres. In a second specimen the crown
presents the sume characters, only that it is flatter on the cinguloid
side. A third specimen has the bevellings on the attached side of
larger extent, so as to reach further down the tooth; but all have
the crown perfectly smooth, without the slightest trace of serrations
on either side. It is quite possible that the bevellings may be
produced by wear, though there is nothing to indicate such an ex-
planation.
Then there are two teeth very similar in character, only rather
broader in the crown, being fully 8 millimetres wide. These spe-
cimens want the bevellings, but have the inner side of the tooth
marked, with a narrow middle surface which may be flat or con-
cave, external to which the tooth is bevelled vertically on one side
and has a thickening at the base of the crown on the other. The
Q. a G. S. No. 148. » U
642 PROF. H. G. SEELEY ON THE REPTILE
base of the cinguloid thickening on the opposite side is convex in
the middle and concave at the sides. Both these teeth are marked
with slight rough ridges (Pl. XXVII. figs. 15, 16), which are not
continuous to the cutting-edge, and are vertical, and much more
marked on one tooth than on the other. Of the two other speci-
mens which have the attached side of the crown flat, one, though
but badly preserved, is remarkable for showing a few faint and
vertical serrations, which are equally marked on both sides (fig. 12).
They did not exceed five in number on each of the cutting-edges,
though only one of these is preserved. All these teeth, I suppose,
may belorg to one species.
There remain two other teeth, which, perhaps, may belong to a
second species or may be worn down. They are characterized
by the same general features as those already described, but had
the crown remarkably low, relatively broad, and hardly making
any approach to a triangular form. ‘The tooth is very thick at
the base of the crown; and the cinguloid thickening extends along
both sides. ‘The crown is smooth, and shows no trace of serration.
I am inclined to refer these teeth to Cratcwomus; they pro-
bably belong to the species described.
Craraomus Pawrtowirscuu, Seeley.
Vertebral Column.
The vertebral column which I refer to Cratewomus is chiefly re-
presented by the tail, of which there are about eighteen vertebrae
preserved ; and the series is very imperfect. ‘There are slight differ-
ences of mineralization in these specimens, some being red, others
brownish, and some nearly black; and there are slight differences in
preservation, since some have the articular margins of the vertebre
rubbed away, and the processes more or less broken, and others
are better preserved but somewhat crushed. Still, when the series
is arranged in sequence there is a perfect continuity of character
and no evidence to suggest that the remains belong to more than
one species, or indeed that they may not all have pertained to a
single individual. A curious feature, also observed in some of the
English Cretaceous Dinosaurs, is the circumstance that these caudal
vertebrae scarcely vary in absolute length, though the centrums
diminish in size. Hitherto no trace of the sacrum has been found.
The dorsal region is represented by two vertebree, which show the
forms of the processes ; while the cervical region is represented by
a vertebra from the hinder part of the neck. In the absence of
evidence of another vertebral column, it may be legitimate to refer
these vertebre to the same species as the tail; and from the
similarity of size it is not unlikly that the whole of these vertebral
remains are the spoils of a single animal, the Crateomus Pawlo-
wrtschia.
Cervical Vertebra.
(See Binzel, pl. ii. figs. 9, 10.)
The centrum and neural arch are both preserved; but the neural
FAUNA OF THE GOSAU FORMATION. 643
spine and transverse processes are broken away. The centrum has
the articular faces somewhat oblique; but though this may be to
some extent natural, it is probably augmented by crushing, since the
form of the centrum has become in this way a good deal distorted.
Its length along the base 1 a) 2,2, inches, while the measurement along
the neural zone: is about ~ inch less. The posterior articular face,
as preserv ed, is ee 13 inch deep, and about 15% inch wide.
It is considerably excavated by a saucer-shaped depression. The an-
terior articulation was probably as deep, and 1,5 inch wide; but it
does not appear to have been so deeply excavated as the posterior
face. The base appears to have been flattened, and margined on
page side by an angular ridge. In the middle these ridges are about
5, inch apart ; and they diver ge towards both anterior and posterior
PE The sides of the centrum are distinctly defined from the
neural arch by the deeply marked horizontal suture, below which
in front is the oblong articular face for the ED; which is about
za inch long and z ce deep. It is about 74 nen behind the
articular ace It rises as a slight pedicle ; and the transverse mea-
surement over these parapophyses is 2,1, inches. The centrum is
compressed from side to side below these } processes, so that a median
cavity divides the side into a highly convex upper portion and a
comparatively flat lower portion. The articular margin of the cen-
trum is moderately sharp, thickened, and rounded. The neural
arch has an aspect of leaning forward obliquely, which is more
marked than that of the centrum, and may probably be taken as
evidence that the neck of the animal was carried in a somewhat
raised position. The pedicles lean forward at an angle of nearly
45°, have their anterior margins concave, and are compressed from
side to side, but especially pinched in the middle. The greatest
width of the arch in front at its union with the centrum is 1,6 inch,
while behind and above the middle of the centrum its w vidth is
reduced to 4% inch, again to become expanded to 13 inch near
the posterior articulation. This median depression extends up to
the side of the neural arch, being margined above and behind by a
sharp buttress, which widens laterally and extends outward so as
to underprop the transverse process, and form with it the upper
head for the rib. Where fractured this process is 1 inch above the
capitular seecuuation, and has a triangular outline pointed in front
and about ;4, inch deep. There is a triangular area which is concavely
excavated behind these transverse processes and in front of the poste-
rior zygapophyses. The posterior zygapophyses are div ed from each
other throughout their length of an inch by a notch 54, inch wide
behind and rather wider in front, where it terminates in the vertical
wall of the neural spine, which in the middle has a slight sharp
ridge. These processes have their inner sides subparallel, are placed
obliquely, and are convex superiorly from below outward. ‘The
articular facets are large, subovate, flat, and look downward and out-
ward soas to make with each other an angle which is more than a
right angle. The anterior zygapophyses extend entirely in front of the
articular face of the centrum. They are similarly divided Ag
au 2
644 PROF, H. G. SEELEY ON THE REPTILE
to a level with the centrum, and are thick strong processes which
have the articular faces somewhat rounded and convex, as though
to allow of considerable play. Behind the facets the bone is a good
deal compressed, so as to be concave in length and concave from side
to side. The base of the neural spine, as preserved, is a square
pillar, rather more than 2 inch in diameter, which appears to rise
vertically. In front of this and between the transverse processes is
a deep excavation about 2 inch long and wide. The neural canal is
large, and formed almost entirely by the neural arch, the neura-
pophyses converging so as to almost unite in the middle line of the
base of the neural cane The width of the neural canal is greatest in
front, where it is 58, inch; and its height is greatest behind, where
it is about the sen, or a little more, the canal being depressed in
front and compressed posteriorly, the width of the canal behind
being +2 inch. The height from the base of the centrum to the
upper surface of the posterior zygapophyses 18 37> 1_ inch; the width
over the outer margins of the posterior zyg gapophy ses is 1 inch ;
the length, from posterior to anterior zygapophyses is 34, inch; the
width over the anterior zygapophyses was about 2>4 inch.
Dorsal Vertebre.
(See Bunzel, pl. 11. figs. 1-3, pl. vii. fig. 24.)
Of the two dorsal vertebre the more anterior has the lower half
of the centrum badly preserved,:but shows the anterior zygapo-
physis, transverse process, and neural:spine completely. In this
the transverse processes extend more horizontally outward, while in
the later vertebra they are directed more obliquely upward To begin
with the latter (Pl. XXX. fig. 3), the centrum is 2,4, inches long, and
has the anterior face subquadrate, 2,1, inches deep, “and 2,5 wide. It
is moderately concave. The posterior face is badly preserved a the
margin, but appears to have been much smaller, since it is 147 inch
deep, and, as preserved, is rather wider. It has a deep pit just below
the eat canal, while the remainder of the face is convex from above
downward, slightly convex from side to side, and smooth. The
neural canal is 2 inches long. The base of the centrum is flattened,
margined by rounded lateral ridges. The upper parts of the sides of
the centrum are concavely compressed, as though squeezed with the
finger and thumb; and here, in the middle of the centrum, the trans-
verse measurementis | inch a little below the neural canal. The neural
arch is lofty, the height to the origin of the transverse process from the
base of the centrum being 3,8, inches, and from its base 2,2, inches.
The buttress which supports the transverse process is flattened at
the side, since it is formed by pillars which arise from the anterior
and posterior margins of the centrum, and converge as they ascend
so as to form a sharp angular ridge beneath the transverse process,
which is flattened and expanded above. There is a deep excavation
in front of the vertical A-shaped masses which support the trans-
verse processes ; and these were placed behind the anterior zyga-
pophyses. There are much larger but similar posterior excayations,
which are subtriangular and in front of the posterior zygapophyses,
FAUNA OF THE GOSAU FORMATION, 645
which were divided from each other, and looked obliquely outward
and downward so as to form with each other an angle which was
much less than aright angle. The neural spine is compressed from
side to side, and originates from a base about 1,4, inch long. The
angle enclosed superiorly by the diverging transverse processes 1s
more than a right angle. The neural canal is subquadrate in front,
and about +7 inch wide, Posteriorly its height becomes 1,3,, and
its width about ;° inch. The neural arch has the aspect of being
placed vertically on the centrum rather towards its anterior
part.
In the other dorsal vertebra the height from the base of the neural
arch to the top of the neural spine is 3; inches. ‘T'he neural spine
is greatly compressed from side to side, be about 15 inch above the
platform of the transverse processes, is 52; inch in its greatest poste-
rior thickness, has an antero- oe “measurement, of 1, inch,
and swells out at its free end to a width of morethan 3 inch. This
inflated mass is convex from side to side, and tapers forward in a
wedge. The platiorms of the transverse processes, which are flat
above and triangular im section, are given out horizontally ; the one
preserved measures 243 inches from the median line to its free end,
which is compressed from above downward, and is rounded from
back to front. The base of this process occupied the whole space
between the posterior and anterior zygapophyses. Its anterior
margin is slightly concave, and terminates in a sharp thin edge.
The posterior side is similarly thin ; but its hinder part is somewhat
broken. ‘The width towards the free end is 1Z inch. On the under-
side is the usual strong median buttress compressed from side to
side, and terminating tonne in an ovate articular facet for the
rib, which is 1 inch long, looks downward and is placed towards
the anterior margin; while it terminates inward abruptly on the
neural arch above in a nearly circular facet, which is large, vertical,
slightly concave, and gave attachment to the head of the rib; half
the facet is above the neural canal. There is the usual superior
concave excavation in front, behind the zygapophyses, while poste-
riorly the concavity which runs along the posterior side of the
transverse process below terminates a an enlarged excavation ;
and these excavations approximate so as to be separated only by a
sharp vertical ridge which is placed above the neural canal, with which
its outline helps to form an §-shaped curve on the right posterior
aspect. ‘The zygapophyses present no peculiarities, the facets being
flat and oblique ; the anterior excavation between the transverse pro-
cesses in front is small; and the interspace between the two facets for
the rib on the sides of the neural arch is about 1} inch. What
remains of the posterior face of the centrum appears to be slightly
concave from side to side, and slightly convex from above down-
ward, though this conditicn has probably resulted from compression.
There is here no sharp line dividing the neural arch from the cen-
trum, though the separation can be easily traced, and it is at the
middle point of the suture that the compression is greatest; there
the transverse measurement is less than Linch. The lower portion
646 PROF. H. G. SEELEY ON THE REPTILE
of Biinzel’s figure of this vertebra is the centrum; the transverse
process is lettered d.
Caudal Vertebre. _
(See Biinzel, pl. ii. figs. 4-8, pl. iv. figs. 6-9, pl. viii. figs. 1, 7, 8, 16.)
There are eighteen caudal vertebre preserved. The earlier ones have
strong transverse processes, which, however, are more or less broken
away, are compressed from above downward, and appear to have been
short ; and the vertebre differ from each other in passing backward in
the suppression of these transverse processes, which become represented
by sharp ridges in the middle part of the series, while towards the end
of the tail all trace of their existence is lost, and the centrum, which
has become gradually reduced in vertical and transverse measurements,
assumes a constricted or dicebox-like outline. None of the caudal
vertebra, except the earliest, appear to have possessed a prominent
neural spine; for the neural arch has well-developed zygapophyses
and a concave outline from front to back. The arch, however, soon
becomes reduced in size, and in the middle of the series is greatly
compressed from side to side, and the articular zygapophysial facets
are lost, while towards the end of the tail the neural arch is a mere
rudiment. The chevron bones were at first apparently large, and arti-
culated with large oblique facets at the hinder margin of the base of
- the centrum; but these facets do not appear to have been quite distinct
from each other, though they were partly divided by the median groove
on the base of the centrum. They soon become relatively small, and
near the end of the tail are quite separated from each other, though
(it may be by an injury received during life) they appear to have become
united to the centrum. Two of the hinder caudal vertebrae are
fractured through the centrum, and show the bones to have contained
central hollow spaces, which, however, were not clearly defined by a
smooth bony lining, but are rather like the medullary cavities of the
long bones of mammals. The articular edges, where preserved, are at
first somewnat rounded, but terminate in a sharp outer margin.
They are very slightly concave, and later on in the series become
almost flat, showing that the tail possessed but little flexibility.
The earliest vertebra preserved has the centrum leaning slightly
forward. It is fully 1; inch long, and the same depth to the
chevron facets on the hinder basal margin, which, however, is badly
preserved. The width of the centrum in front, at the base of the
transverse processes, is 1,J, inch. ‘The corresponding width behind
is a trifle less. The anterior articular faco is nearly flat, but had
the margin rounded. ‘The posterior articular face is more concave,
and the rounding of the margin is less marked. The upper borders
of the transverse processes are on a level with the base of the
neural canal. They are placed nearer to the anterior than to the
posterior articular face, are transversely oblong where broken close
to the centrum, and measure ;°, inch in length, ;4 in depth. Be-
low them the centrum is compressed ; the base is broad, ill defined,
1 inch in width, rounds into the sides, and is divided longitudinally
by a shallow groove about ;3, inch in width, which is most marked
FAUNA OF THE GOSAU FORMATION, 647
posteriorly. The neural canal is high and narrow: the sides of the
neural arch converge upward ; and the anterior zygapophyses have
the facets looking inward; they are concave in depth.
The second and third vertebre of the series only differ in having
slight tubercles adjoining the anterior and posterior articular margins
on the middle of the sides, and in the decreasing dimensions of the
centrum and processes, though the length still remains the same.
The fourth vertebra is distorted by vertical compression, and the
fifth by lateral compression. It, however, has the neural arch well
preserved, and shows the length from the anterior to the posterior
zygapophyses to be 213 inches. There is also an indication of a slight
neural spine broken away, which rose above the posterior zygapo-
physes. The greater part of both anterior and posterior facets pro-
jects beyond the centrum. The anterior pair of facets is divided
from each other ; but there is only a slight notch at the hinder ex-
tremity of the posterior pair. In the sixth vertebra the neural
arch is seen to taper posteriorly, when seen from above, in a trian-
gular outline slightly compressed in the middle; and in the seventh,
in which the centrum is 1,8, inch long, 1,4, inch deep posteriorly,
and slightly wider, the neural arch is 2,4, inches long. There is a
distinct concave compression below the anterior zygapophyses, from
which faint ridges extend backward longitudinally towards the pos-
terior zygapophyses. ‘The facet from which the transverse process
has come away is still ovate, about ;4 inch long, and is placed in the
middle of the side of the centrum, just below the neural arch. The
neural spine is seen to be a slight sharp ridge. The anterior zyga-_
pophyses are 41 inch apart, while the posterior zygapophyses, which
have smaller facets, are 54, inch long. The groove on the base of the
centrum has become somewhat narrower and more sharply defined.
Here several vertebrae appear to be missing ; and in the next of the
series the transverse process has become much smaller, is placed lower
on the side of the centrum, is margined by a vascular groove in front,
and is prolonged backward by a sharp ridge towards the articular
margin. The vertebre now begin to elongate a little ; and the ninth
of the caudal series is 1,9, inch long; the transverse processes have
disappeared, and are only marked by a sharp median ridge in the
middle of the centrum, margined in front by an oblique vascular
groove. Above these lateral ridges the centrum is compressed from
side to side; the basal groove has become much shallower and
best marked towards the extremities. The tenth and eleventh show
the neural arch to be greatly compressed from side to side, and to
rise very much higher behind than in front, owing to the greatly
diminished size of the anterior zygapophyses. The posterior zyga-
pophyses have disappeared; and the centrum is a good deal constricted
in the middle. The twelfth centrum shows a much greater reduc-
tion in size of the neural arch, which leaves the posterior third of the
centrum free. The underside of the centrum is similarly compressed
to the upper part, though the median basal ridges become rounded.
The facets for the zygapophyses are distinctly marked at both ends,
and divided by a groove, of which there is no trace in the middle of
648 PROF. H. G. SEELEY ON THE REPTILE
the base. In the thirteenth and fourteenth vertebra the centrum
is 1,5 inch long, with the articular face 1,4, inch wide in front and
rather less behind, while the depth in front is 1 inch. The neural
arch is small, andits superior outline horizontal. The measurement
from the middle of the base of the centrum to its upper border is
1, inch. The neural canal indents the centrum concavely at both
back and front articulations ; and from the hinder limit of the neural
arch a vascular groove impresses the sides, descending slightly for-
ward to the middle of the base. The centrum here is most con-
stricted, and measures 55, inch from side to side, and has a rather
less depth. The chevron bones are preserved in the thirteenth ver-
tebra, with the posterior margin of which they appear to be blended;
they unite below in a Y-shape, and have facets for the succeeding
vertebra. They are $2 inch wide, $} inch deep, and, with the
groove at the terminal end of the centrum, enclose the vascular
canal. Of the fifteenth vertebra only half the centrum is pre-
served. ‘The sixteenth and seventeenth are blended together, and
the chevron may not have united in the median line. The vertebree
now become roughened with many slight longitudinal muscular
ridges, indicative of the near approach of the end of the series; and
the articular faces of the centrum appear to have central con-
cavities.
Ribs.
(See Bunzel, pl. iii. figs. 5, 6, pl. viii. figs. 14, 15, pl. 1. fig. 27.)
One cervical rib is preserved ; there are about half a dozen tolerably |
perfect dorsal ribs, and a multitude of fragments of dorsal ribs. The
majority of these obviously belong to one animal; and I refer them
to the smaller of the two large Dinosaurs, Crateomus lepidophorus ;
but there are a few slightly larger fragments which possibly pertain
to the larger Dinosaur. They are, however, too imperfect to yield
any characters for description; and as they are doubtful remains, I
prefer to leave their elucidation to future discoveries. They are
larger and stouter than the bulk of the specimens. ‘The only ex-
ample which shows the proximal end is represented in Pl. XXX1.
fig, 12, and may be compared with the corresponding part of the
smaller rib, fig. 17, Pl. XX VII. This proximal end is the speci-
men figured by Biinzel as the lower jaw of a lizard, a determination
which is presuniwviy due to its imperfect condition and the cireum-
stance that the transverse platform is only developed on one side.
I owe its identification to Mr. Hulke, who recognized its resemblance
to the smaller specimens when examining the collection.
The cervical rib wants the articular head of the lower tubercle.
The interspace between these two heads was nearly 13 inch, the
outline between them being deeply concave; the ventral outline is
flat, the dorsal outline concave. The length of the rib, as preserved,
is 3,2, inches. After being directed outward for half its length, it
curves concayely backward and tapers at the same time. There is
in front, in the middle of the rib, a slight ridge. The articular head
which is preserved is 58; inch long and ,% inch wide. When perfect
eT
marine Sok 15
—
:
.
*
t
.
n
9)
FAUNA OF THE GOSAU FORMATION, 649
the rib must have had a Y-shaped form ; and just below the fork
of the Y on the posterior side is a moderately large vascular
foramen.
The dorsal ribs are all imperfect at the distal end; and some of them
have a much greater curve than others. The longest fragments are
imperfect, proximally and distally, and measure round the outside
curve about. 1] inches, and across the chord a little over 10 inches.
But all the ribs agree in distinctive character, which is seen in side-
to-side compression along the proximal half of the visceral surface
and lateral expansion on the dorsal surface (Pl. AXVII. fig. 17),
so that in this haif of the rib the transverse section is shaped
like a 7 (Pl. XXVIII. fig. 18); but distally the rib expands
on the visceral surface, and the elevated ridge on the ante-
rior border disappears, the direction of the rib becomes some-
what oblique, and its section has a compressed ovate outline. One
consequence of this remarkable dorsal expansion is to form an ex-
panded table-like external surface which is convex in the direction
of the length of the rib, and nearly flat in the antero-posterior
direction ; so that the ribs closely resemble the combined rib and
costal plate of a Chelonian, and in the living animal the interspaces
between the ribs must have been as small as in many mammals, such
as the Buffalo and the Lesser Anteater. It is, of course, possible that
this expansion of the dorsal margin of the rib may be homologous
with the costal plates of Chelonians, since representatives of the
structure are also met with in Crocodiles, Hatteria, and birds. I
have no doubt that this table structure carried the heavy dermal ar-
mour with which these animals were weighted. One specimen (fig. 17),
which has the articular head preserved, has an interspace of 13, inch
between the capitulum and tuberculum. The capitulum curves
slightly forward, is $+ inch in depth, and gradually widens on the
ventral surface towards the articulation, where it is 4 inch in dia-
meter. The tuberculum is relatively small, } inch from back to front,
and about 4 inch in width. It is somewhat reniform and rounded,
like the outside of a kidney. Immediately beyond the tubercle the
bone begins to widen ; and the anterior ridge extends in the speci-
men 4 inches, while in other ribs it extends 6 inches, and in
some only 3. Its antero-posterior width is also variable, but,
where widest, in no specimen measures more than | inch, and is
usually about #inch. The compression of the rib just below the
tubercle gives a measurement of less than ;%, inch, though in some
specimens it may be a little more and in others less ; while the depth
of the rib from dorsal to ventral surface is at first ;?, ich, and be-
comes gradually reduced as the rib extends and loses its T-shaped
section. ‘The side-to-side compression extends close under the ex-
ternal platform, so that both sides of the rib are concavely chan-
nelled. Several specimens show some amount of muscular roughness
on the transverse platform and a part of the rib distad to its termina-
tion ; and this is probably correlated with the muscular attachment of
dermalarmour. The longest ribs preserved do not indicate a greater
length when complete than 14 inches. When they become obliquely
650 PROF. H. G. SEELEY ON THE REPTILE
flattened they maintain a remarkable uniformity of width, and taper
almost imperceptibly towards the distal extremity.
Dermal Armour.
(See Btinzel, pl. iv. figs. 1, 2, pl. vii. figs. 20, 21, pl. vin. figs. 9-12.)
The Dinosaurian dermal armour which I refer to the genus
Cratwomus presents many remarkable modifications, such as have
not been met with in any genus hitherto described. Some of the
plates are remarkably similar to those of Scelidosaurus and <Acan-
thophols; others are large scutes with a median longitudinal ridge
and numerous vascular impressions on the carinate surface, as
though they were imbedded in the skin. These plates are all
thin and may have been abdominal, while the more elevated plates
may have been dorsal and caudal. A third type of plate appears
to be greatly compressed from side to side with a sharp cutting
surface in front, terminating in a spike superiorly, and with a
rounded posterior margin. The articular bases of these plates are
not preserved. A fourth kind of plate of large size appears to have
terminated at each end in a great triangular spike, while across the
intermediate space there extended rows of conical tubercles some-
what resembling in outline those attributed to Hyleosaurus. A fifth
kind of armour is represented by an immense conical spine, like the
horn-core of an ox, which rises from a bony base.
None of these pieces of armour are symmetrical, hardly any of them
can be grouped in pairs ; altogether there are fully fifty well-defined
plates, besides a large number of fragments. It is quite possible
that the remains may have belonged to more than one species. But
seeing that the vertebral column of one species is well preserved in its
hin dey portion, andthatto this species the bulk of the limb bones may
reasonably be ‘relegated, and that in many points of osteology there
is an approximation of the animal towards Scelidosaurus, we may
be justified in considering that the larger Austrian Dinosaur possessed
armour as varied in character as that seen in its English prototype ;
and in the absence of a second and larger vertebral column, I am
unwilling to attempt to divide the scutes between the two different
animals, merely on the ground of their contours. Yet it may be
acknowledged that the horncore-like scute is larger than would
have been expected, and that the whole armour is heavy even
for an animal with such strongly marked muscular development as
is shown on the bones of the limbs of both the species.
I proceed to describe the armour according to the varieties it
presents. As Prof. Suess had noticed, there is, besides the horn-
like scute, a second base, from which the horn-like spine has been
broken away. There thus appear to have been at least a pair.
The base from which the horn rises (Pl. XX VIII. fig. 4) 1s 55 inches
long, of irregular oblong shape with roughened edge, a little
oroken at one end. It is nearly 33 inches wide where widest,
and narrows to about 23 inches. It is concave in length on the
under surface in the middle, convex at the sides. The margin is
full of vascular perforations, and appears to have had strong union
FAUNA OF THE GOSAU FORMATION. 651
with the skin. On the broad side this bony base is 1,8, inch thick ;
on the narrow side the greatest thickness is 1,4, inch. The horn-
like spine is placed obliquely upon it, and rises vertically, curving a
httle backward or outward. It is 53 inches high. Its base is ra-
ther more than 23 inches long, and 2,1) inches wide. ‘The spine is
slightly flattened on the convex and concave sides. ‘The right
and left sides are nearly straight. The bone is covered with close-
set irregular vascular perforations similar to those on a horn-core.
(See Biunzel, pl. v. fig. 10.)
Two other plates of quite as remarkable character are dissimilar in
form, one being twice the width of the other; but both had smooth
bases for attachment to the skin. The base is rounded at its lateral
margins, as though it were a bone distinct trom the extraordinary der-
mal ornament which rises fromit. The larger specimen (PI. XXVIII.
fig. 2) is 8 inches long and imperfect at one end. The articular base
appears to have been about 43 inches long and 2 inches wide, while
the greatest width of the plate is 3} inches towards each end of the
articular space, and in the intermediate area it becomes contracted
to about 24 inches. The spine which existed at the other end of this
contracted area has been almost entirely broken away ; so that the
plate was originally probably a central oblong mass with constricted
sides terminating at each end in a large triangular spine, which was
directed upward from the body of the plate. The one spine which
is preserved is on its upper surface about 4 inches long, and at
the base 3z inches wide. It is slightly convex from side to side,
and terminates in a sharp cutting-edge on each side, which is lon-
ger and more convex on one side than on the other; and the longer
edge is reflected a little upward. There are a few longitudinal sub-
parallel vascular grooves in the middle of this part of the plate. On
the under surface of this region the bone is flattened on the two
sides, which converge towards a rounded ridge in the middle line,
which helps to give strength to the sharp dagger-like extremity in
which the bone terminates. The greatest thickness of this part
of the plate in the middle is 1/ inch. Its base terminates
abruptly, perhaps owing to some crushing on the underside. The
middle oblong portion of the plate is studded over with conical tu-
bercles, the bases of which are pretty clearly defined, and the cones
are low. ‘They are arranged across the bone in three rows with
four low conical tubercles in each of the two outer rows and
two larger tubercles in the middle, 1 inch in diameter, with three
on the external margin of each, making in all 6 in the middle.
These tubercles make an elevated border abutting against the tri-
angular spine. Their surfaces are roughened with close-set irre-
gular vascular punctures. The smaller plate (Pl. XXVIII. fig. 3),
of similar character, is rather better preserved, its total length
64 inches, length of the articular base 54 inches. It carries a
vertically elevated spine, and the base beneath this is deeply con-
eave. The margins of the base are smooth and well rounded as
already described in the larger specimen. The width of the base
is 13,inch. At one end the compressed spine rises at an angle
652 PROF. H. G. SEELEY ON THE REPTILE
from the part of the plate on which it is situate; it is somewhat
fractured ; but its height as preserved is nearly 23 inches, and the
length of its base rather less; it terminates towards the free extre-
mity in a sharp cutting-edge. Its thickness in the middle of the base
is 5% inch; and it tapers upward and outward towards both margins.
It is defined at the base by a constriction which appears to separate
it from the plate from which it rises.* It is scored with somewhat
irregular vertical vascular furrows. The corresponding plate at the
other end is much smaller, and is defined from the under articular
surface by a furrow; and a similar furrow appears to mark its mit
on the upper surface, as though it did not completely cover the bone
upon which it rests. It is of ovate outline, 2,4, inches long and 1}
inch wide in the middle. Its surface is undulating, as though the
free extremity, growing against another plate, had been forced up
into an elevation. It has the aspect of projecting on one side be-
yond the bone on which it rests, and is then sharply compressed, and
terminates in a cutting-margin which is convex in length. The in-
terspace between these terminal plates is rhomboidal, about 1,% inch
in length, and is covered with conical tubercles, the largest of which
is +5 inch long and about 4 inch high. These tubercles are about
© in number, the 3 largest being on one side.
The next series of dermal bones are all longitudinally carinate.
They may, perhaps, be divided into such as have the base angularly
excavated, as though they were median bones of the dorsal or
caudal region, and such as have the base comparatively flattened ;
and in these latter the keel becomes greatly reduced in height:
these bones are probably lateral. Judging from the example of
Stagonolepis, I am inclined to believe that most of these plates
pertain to the tail. There are four plates, each about 2%, inches
long, with an ovate base having a rough margin, rising into a sharp
cutting median keel about 2 inches in height, which has a ver-
tical sharp margin behind and a convex margin over the length
of the plate (Pl. XXX. fig. 2). The sides of these plates are con-
cave from above downward, and convex in length; but they are
all somewhat distorted by pressure. They thin away at the free
margin to about ;4 inch in thickness. our other plates, also an-
gular on the underside, are much more elongated, and clearly over-
lap each other at one end, which may be presumed to be posterior.
The largest of these plates is 6? inches long, 14% inch wide where
widest behind, and 24 inches high in the highest part of the sharp
compressed keel. One side of this plate is moderately concave from
above downward; the other side is plano-convex;. and posteriorly the
underpart of the bone has the aspect of being obliquely truncated—
a character which results from the posterior 23 inches rising free
from the basal attachment so as to terminate in an upward and
backwardly directed spine, which overlapped the next succeeding
plate. The crest of the median ridge has a very slight sigmoid
flexure. Attached to this bone on one side is a small fragment
which appears to be a broken portion of the proximal end of the
dorsal rib. Other plates are somewhat flatter and relatively broader ;
FAUNA OF THE GOSAU FORMATION. 653
one which measures nearly 5 inches in length has a subrhomboidal
outline, two long sides converging in front, and a short pair of sides
converging behind. The greatest width of the plate is 23 inches.
The greatest length of the flat part of the base is 32 inches ; and
the posterior 14 inch rises into a strong spine, which terminates the
median crest, is 1,%, inch high, compressed behind and above. The
crest gradually diminishes in height from this spine forward till it
dies away at the anterior end. The outline of the crest is very
slightly sigmoid. The crest has a compressed aspect, as though it
had been naturally squeezed from side to side in its upper half.
There are numerous smaller sharply carinate plates of a some-
what ovate outline, with the keel placed nearer towards one margin
than the other, and always becoming a little more elevated towards
one end, where it is truncated. And these plates, though mostly flat
on the underside, always have the end on which the ridge is highest
bent a little upward, as though to overlap the next succeeding plate.
These plates vary in size: one is 2,8, inches long, 1,5, inch wide,
and has the keel $4 inch high ; another is 2-3, inches long, 1,4, inch
wide, and has the keel 55, inch high posteriorly.
Another remarkable series of plates is distinguished by extreme
thinness. They appear all to have been subrhomboidal and to have
had the keel scarcely elevated.
The largest is about 2,5 inches long, and more than 2,%, inches
wide. The under surface is smooth and slightly convex. The su-
perior and inferior margins converge to a sharp but irregular edge ;
the thickness of the body of the plate is about 4, inch, though many
of the plates are much thinner; and the thickness in the line of the
median ridge is about ;#; inch. This slight keel does not extend to
either extremity of the plate; but the margin of each plate is turned
up towards one of the posterior sides, as though they still obliquely
overlapped (Pl. XXXI. fig. 3). The surface of these plates is
slightly concave on each side of the median ridge, and there scored
with vascular markings which ascend towards the ridge and ramify
and interlace. ‘Their prevailing direction in the plates with more
elevated keels is towards the posterior spine. There are a few
slightly thicker plates which have no trace of keel, but are flat
below and gently convex above (Pl. XXVIII. fig. 5), with a deep
Y-shaped vascular groove on each, and a sharp margin. The
smallest and best-preserved is 1,4 inch long, and 1,1; inch wide.
Some fragments of crest-spines, broken away from the bases, in-
dicate plates of a larger size than any thing here described. The
plates appear to have been remarkable for their great side-to-side com-
pression, the posterior elevation of the crest, and the sharpness of
the spine, which, in fragments preserved, extended to a height of 5
inches where the antero-posterior measurement is only about 3
inches, and the greatest thickness of the spine from side to side is only
42 inch (at the interior fracture).
There is also a fragment indicating that the plates in which the keel
is almost suppressed, in some regions attained a larger size than has
here been described.
654 PROF. H. G. SEELEY ON THE REPTILE
One such fragment as preserved is about 5 inches long and rather
wider, with apparently two slight keel-like ridges parallel to each
other. The greatest height of the crest in this specimen is about
45 inch.
* If all this armour is correctly referred to the genus Cratwomus,
it furnishes one of the most distinctive generic characters of this
type. I do not remember any described genus in which large
tubercled plates such as are here figured have been found, though
an isolated plate was described from the Wealden of the Isle of
Wight many years ago* as showing a not dissimilar ornament.
Other plates are so similar to armour of Scelidosaurus, especially the
median-keeled caudal plates, as to enable us to concur with Biinzel
in recognizing a strong affinity to that genus, which, however, does
not amount to identity. Cratewomus was more heavily armoured.
It is difficult to say whether its armour has more in common
with the bony tubercles which occur on the limbs and tail of many
Chelonians, or approximates better to the bony scutes of certain
lizards and crocodiles; for it is so distinct that no near parallel
can be drawn between the armour of Dinosaurs and that of living
reptiles; nor if the comparison were possible would it have much
weight as a mark of organic affinity.
Scapule.
Three specimens of Dinosaurian scapulex have been obtained ; two
are larger than the other, and belong to a distinct species. The two
larger specimens were figured by Bunzel, and regarded by him as
left ribs of his imaginary Lacertilian genus Danubiosaurus and the
type of his species D. anceps. ‘They are left scapule. The smaller
specimen obtained subsequently is a right scapula. I refer the.
larger bones to the animal indicated by the larger limb-bones (Cra-
teomus Pawlowitschir), though, as the smaller specimen is little more
than half the size, the disproportion in the scapule is much greater
than would have been anticipated in the two species.
Left Scapula.
(See Bunzel, pl. v. figs. 7-9, pl.vi. figs. 1-3.)
The scapula (fig. A, p. 656) is remarkable for its great breadth, its
curved form, its compressed aspect, and the remarkable acromial pro-
cess in which its slight spine terminates. The specimen has been a
little crushed, and is not quite perfect at its distal end; the whole
surface for union with the coracoid is destroyed by decomposition, and
slightly injured by fracture. What remains of the articular surface
for the humerus is a semiovate surface 54 centim. wide and rather
longer. Itis margined by an elevated ridge, has the usual roughness
of cartilaginous surfaces, andis more concave than usual, both in length
and breadth. The inner or visceral margin of the bone appears
to have been more convex than the external margin. Both are
somewhat inflated; and the external surface and posterior margin
* J. H. Lee, Ann. & Mag. Nat. Hist. vol. xi. p. 5, reprinted in his ‘ Note
Book of a Geologist.’
FAUNA OF THE GOSAU FORMATION. 655
especially are roughened with ligamentous attachments and mus-
cular rugosities. The thickness of the bone rapidly “diminishes
above the articulation; and it continues to become thinner towards
the free end, where the thickness does not exceed a centimetre
and a half. The posterior margin is compressed and rounded,
the rounding becoming more conspicuous as the surface ap-
proaches the humeral articulation, owing to the increasing thick-
ness of the bone. The length of the posterior side of the bone is
about 25 centim.; its outline is concave; the concavity, as preserved,
may be indicated by the fact that the chord joining its two ex-
tremities is 2] centim. long, and the abscissa 6 centim. high. The
corresponding anterior margin is not quite parallel, since the bone
is wider in its upper third than in its lower third; and hence the
‘anterior margin is more convex. ‘The least transverse measurement
above what may be termed the spine of the scapula is 63 centim.
In the upper third of the bone the width has increased to upwards
of 8 centim.; it then contracts a little to less than 8 centim., so as
to make the anterior termination of the superior margin concave;
for the bone widens once more, so as to become broader than ever
at its free end. The posterior corner of the free end appears to
be curved a little outward. The external surface is smooth, con-
vex in length, and more convex in breadth at the distal end than
proximally. The visceral surface exhibits corresponding characters.
The anterior margin of the bone is thicker, better rounded than
the posterior margin, and rougher with muscular attachments. As
preserved, the measurement from acromion to the anterior distal
margin is 23 centim. in a straight line. In about the middle of
the anterior margin the bone becomes appreciably thickened on
the inner side with muscular attachments, and the thickness in-
ereases until a vertical anterior shoulder is formed almost at right
angles to the spine of the scapula, extending downward and inward
towards the coracoid area. Only a small portion of this trian-
gular space is preserved; but so much of it as is seen below the
acromion is 4 centim. deep. The spine of the scapula only runs for
a short distance along the proximal part of its surface, and is diffi-
cult to define, because the bone is obviously compressed so as to
make the surface posterior to the spine appear more concave than
it really was; but the spine may be considered to originate in
the thickening of the anterior margin of the bone already alluded
to; and it becomes most distinct a centimetre or two above the
acromion, where it is 13 centim. wide, flat above, and margined at
the sides by rounded ridges. It is prolonged into a free process or
acromion, which was directed forward and outward. This process is
a little crushed, is nearly 5 centim. long, 33 millim. broad, and, as
preserved, about 2 centim. thick, though before crushing it was
thicker ; the corners and angles of its free end are rounded; and
the inferior or internal surface is concave, since it rises from the
anterior coracoid border of the bone. The plane of the acromion is
parallel to that of the blade of the scapula, and makes an angle of 45°
with the direction of the humeral articular surface. The distance
656 PROF. H. G. SEELEY ON THE REPTILE
Scapule of Crateeomus Pawlowitschii and C. lepidophorus.
Wi
/
A. Left scapula of Crateomus Pawlowitschii.
B. Right scapula (drawn reversed for comparison) of Crateomus
lepidophorus.
1. Humeral articulation. 2. Acromion process.
FAUNA OF THE GOSAU FORMATION, 657
of its inferior border from the humeral articular surface is between
6 and7 centim. From the inferior margin of the acromion descends
a strong rounded ridge which divides the part of the bone above the
humeral articulation into anterior and posterior areas, and, but for
the intervening acromion process, would look like a continuation of
the spine. This ridge dies away before reaching the humeral arti-
culation. Posterior to the acromion the surface of the scapula is
broadly channelled. In its singular curvature and development of
the acromion it is unlike the scapula of any other Dinosaur.
‘he second specimen, though evidently belonging to the same spe-
cies, is a little smaller; it has been reconstructed out of even a larger
number of fragments than the specimen described. The proximal
part of the bone is wanting, the fracture having removed the arti-
cular region and acromion process ; but this portion was compressed
from side to side; the anterior margin of the bone, however, appears
to be thicker, and the cavity in front of the acromion is more
marked, than in the specimen here figured. Distally a portion of the
terminal free margin of the bone is preserved, showing that it was
obliquely truncated and somewhat thickened and roughened with
muscular attachments, especially towards the posterior border; the
specimen, as preserved, is 27 centim. long and about 76 millim.
wide in the blade, where it is widest. The details of the two bones
otherwise present the closest agreement.
Distal End of Humerus.
A large humerus is unfortunately only known from its distal end
(Pl. XXIX. fig. 4), which has decayed in the manner so frequent
with these fossils, and as though indicating that the terminal end
had been a distal epiphysis similar to that which characterizes the
long bones in the order Sauropterygia, which may have separated
from the shaft absolutely or decayed in consequence of the less per-
fect ossification of its cartilaginous substance.
This fragment is little more than 4 inches long. It exhibits at
the proximal end a natural fracture, made during extraction from
the rock; and here the bone is 1,8, inch thick, 1,5, inch wide, ovate
in outline, with an angular bulge towards the middle of the superior
surface—a bulge which indicates a ridge similar to that referred
to in the more perfect specimens of the other species (Pl. XXIX.
fig. 1). I regard this specimen as the distal half of a left humerus
of Cratwomus Pawlowitschi.
The fracture is somewhat interesting as showing the existence
of a central medullary cavity (Pl. X XIX. fig. 5). This cavity is
= inch long and more than 3 inch wide; so that the bone round
it is about half an inch thick; and this contrasts remarkably with
the thinness of the terminal and irregular edges of the distal margin
of the shaft, which is nowhere much more than ;y inch thick, though
becoming somewhat thicker as it extends proximally. The cavity
is relatively smaller in the second species. The superior surface is
unfortunately somewhat crushed; and the whole specimen has been
pieced together, like so many of these remains, with great patience, —
Q.J.G.8. No. 148. 2x
658 PROF. H. G. SEELEY ON THE REPTILE
skill, and success. The shaft does not widen quite so rapidly towards
the distal end as in the smaller species, since the bone is 24 inches
wide only at 24 inches further towards the distal extremity. The
surface is remarkably smooth and free from muscular markings,
except on what I regard as the outer side. This is roughened; and
rather above its middle there is a chain of strong muscular eminences
(which appear to be much in the position of the inner straight ridge
described in Crateomus lepidophorus, in which, however, the ridge
was only developed proximally). Here it is strong distally, and
would seem to have extended to the terminal articulation. The
middle of the inferior aspect is marked by a straight vascular groove
about an inch long in the upper half of the fragment; and at the
extreme distal margin towards the inner side there is a vertically
ovate muscular pit about 1 inch long. The distal extremity appears to
be curved downward and outward rather more than usual, while the
surface is more than usually convex. The sides, which are slightly
concave in length, are comparatively straight. The extreme width,
as preserved distally is 3 inches; but this is fully 1 inch short of
what must have been the end of the specimen.
Femur.
(See Bunzel, pl. iii. figs. 2-4.)
The shaft of the right femur which I refer to this species is very
well preserved ; but there is no trace of the articular extremities,
which disappeared before the bone was imbedded in the matrix ;
and towards the articular ends the bone is crushed, on the posterior
aspect proximally, and at the distal end in front. There is, how-
ever, quite enough preserved to indicate a very distinct animal from
that referred to Cratwomus lepidophorus (Pl. XXXI. fig. 5), to
which, however, it was nearly related in femoral character. The
fragment (PI. XX XI. fig. 1) is 11 inches long and 1,4 inch wide
in the lower third of the shaft, is remarkably cylindrical, has the
muscular ridges on the anterior surface strongly developed, while
the inner middle trochanter of the shaft would not be recognized as
such, so feebly is it developed, were it not for the characters of the
other species. As preserved, the appearance of the bone is remark-
ably mammalian. When perfect, it may have been 15 inches long.
The fragment of the corresponding left femur is scarcely at all
compressed, but was so far destroyed before mineralization that
only 7 inches of its length now remain, showing the lower half of
the shaft to be subtriangular in section, being flattened behind and
somewhat compressed towards the median muscular ridge in front.
The following description is drawn from the representative of the
right limb (Pl. XXXI. fig. 1). The bone, which is most constricted
in the lower third, widens in the usual way towards both proximal
and distal ends; and its most remarkable feature is the inflation of
the proximal half of the dorsal or anterior half of the shaft in the
line of the median longitudinal muscular ridge. This ridge is strong ;
and its crest is broken into short lengths of from half to three quarters
FAUNA OF THE GOSAU FORMATION. 659
of an inch; it originates distally in the part of the shaft which is most
constricted, runs rather nearer to the external than to the internal
margin, and increases in strength proximally till it becomes 52, inch
wide, where the shaft is 3 inches in diameter. All that part of the
shaft which is external to the ridge is obliquely flattened, with a
slight increase of inflation towards the proximal end, but without the
slightest indication of the formation of a proximal trochanter, which
presumably was not developed, though the absence of this struc-
ture may be due to mutilation. The inner side of the shaft is rather
more convex than the outer side ; but on its upper side there curves
round from where the lateral trochanter should be, a muscular ridge,
which is rather stronger but less well defined than the principal
median ridge, towards which it very slowly converges proximally.
At first the width between the ridges is nearly 14 inch: but at
3 inches nearer to the proximal end it is narrowed to 1,1, inch; and
as it narrows, the area thus defined between the muscular ridges,
which is at first flat, becomes very markedly concave. Proximally
the bone curves inward as though approaching the terminal arti-
cular head, and the space external to the inner ridge is fairly well
rounded. The proximal half of the posterior aspect of the bone is
somewhat crushed, and appears to have been more convex than
usual. It may have terminated towards the outer side in a slight
ridge, and shows but very slight or uncertain indications of the
posterior muscular ridge seen in the second species. The lateral
trochanteroid muscular indication is placed a little higher up than
is usual with the lateral trochanter ; itis about 1} inch long, slightly
elevated and rounded; its proximal end inclines slightly towards
the anterior face of the bone. The lateral outline of the bone is
here markedly convex.
The distal end of the bone gives no indication of the widening
on the outer side of the articulation which is so often met with,
since it is flattened and straight externally. Posteriorly there is
a moderately deep broad channel inclined a little outward; it was
evidently prolonged between the condyles, and shows the outer
condyle, as usual, to have been small, while the inner condyle was
large. The bone appears to have been quite as much thickened as
usual at the distal end, though only the backward curve of the shaft
and no part of the articulation itself is preserved. The whole sur-
face of the shaft is remarkable for the longitudinal muscular rough-
nesses, which are more marked than in any reptile bone that I have
ever seen.
Tibia.
A pair of large limb-bones, both 8 inches long, as preserved, but muti-
lated before fossilization, so that no trace is shown of either proximal
or distal articulations, present, however, characters which unmista-
kably show them to be the tibial bones (Pl. XXXT. fig. 2). The frag-
ments are straight on the inner side. The shaft bends inward a little at
the distal end, has a long anterior crest immensely developed forward
at the proximal end, and sends out a compressed process on the outer
2x 2
660 PROF. H. G. SEELEY ON THE REPTILE
side. The bone measures from back to front at the proximal end 38
inches, while the middle of the shaft measures 18 inch, and the distal
end 1finch. The whole inner surface is remarkably flattened, and,
except for the usual distal widening, shows no character that calls
for remark. ‘The posterior aspect is badly defined, somewhat flat-
tened towards the distal end, where the bone is rough with muscular
markings, and 17 inch from side to side. The thickness in the
middle of the shaft is apparently less, though the bone may be some-
what compressed ; and the thickness varies in the two specimens. In
length, the posterior outline is slightly concave in the middle of the
shaft, and slightly convex in its upper portion, where it is well
rounded from side toside. The outer surface of the bone is convex
from back to front, and slightly concave in length. It becomes
compressed proximally ; so that it is divided by an elevated median
ridge into two portions——_the posterior somewhat flattened and look-
ing obliquely outward and backward, while the anterior half is
deeply concave, the concavity resulting from the natural compres-
sion of the shaft anteriorly, so as to form an immense patelloid
crest something after the pattern of that figured by Leidy as cha-
racterizing Celosaurus. The anterior margin is somewhat sharp,
and is defined at the distal end by a slight angular ridge, which above
the middle of the shaft extends inward; so that the proximal por-
tion of the anterior outline becomes convex from side to side, though
the side-to-side compression increases, and the bone, where frac-
tured, is again increasing in width from side to side, and measures
4 inch. The upper part of the shaft has a subtriangular section,
owing to the elevation of the external or fibular ridge. Fibule of
two sizes occur; but the larger specimen is so small that I have
noticed it under the next species.
CRATHOMUS LEPIDOPHORUS, Seeley.
In.grouping together the remains which are now to be described
I have been influenced partly by their anatomical characters, partly
by size, and partly by the fact that I have no evidence of the limb-
bones of a third species of the same genus to which any of the
bones might be referred. The specific distinctness of this smaller
Dinosaur will be found well indicated by the characters of the
scapula, humerus, femur, and vertebra. ‘The armour is probably
undistinguishable from that of the larger species; and at present
there is no sufficient ground for saying how much of that already
described belonged to Cratwomus lepidophorus.
Left Coracoid.
(See Bunzel, pl. iv. fig. 3.)
The left coracoid is very imperfectly preserved, giving no indica-
tion of the outline of the bone, no trace, or even indication of direc-
tion, of its union with the scapula, and showing the articular surface
for the humerus but imperfectly. The bone, however, is perfectly
recognizable; it has been figured by Biinzel as the right side of
the ilium of Zguanodon Mantel. Since no other example of a
FAUNA OF THE GOSAU FORMATION. 661
Dinosaurian coracoid occurs in this formation, it may be useful to
record the few indications and characters which it displays. The
length of the fragment is about 113 centim.; its breadth is 44
centim. I infer it to have been a bone, however, fashioned on
the plan of the coracoid of Hyleosaurus or Scelidosaurus. The bone
thickened considerably towards the articular surface for the humerus,
where the greatest transverse measurement is 36 millim., though,
being eroded, this may not have been its widest point. The length
of the articulation is about 65 millim.; but, from the state of preser-
vation of the specimen, this can only be given approximately. There
are some irregularities on the surface which would suggest car-
tilaginous covering, such as is indicated by the articular end of
the scapula. In length, the surface is slightly concave. Below
the articular surface the bone is excavated concayely in length,
though the excavation is not very deep. This inferior surface is ob-
liquely compressed on the inner side, so that a slight and rounded
ridge extends downward from the articular surface on the outer
margin of the bone. The excavation extends slightly under the
articular surface. ‘The visceral surface is so eroded as to be almost
unrecognizable, only one or two patches of unworn bony surface being
preserved. The external aspect towards the scapular articulation is
roughened with longitudinal ridges. The middle part of the bone
appears to be smooth, but carries a row of seven or eight vascular
pits close to the elevated and compressed margin of the humeral
articular surface, in front of which is a broad shallow furrow, as
though the thumb had been drawn over a plastic substance. This
furrow becomes wider as it extends downward, and at its distal termi-
nation is margined by shght muscular rugosities. Distant 3 centim.
from the upper part of the humeral articulation, and rather more,
apparently, from the margin of the scapula, was the coracoid foramen,
which was about 15 millim. in length and probably ovate or pear-
shaped, though its outline is imperfectly preserved. The external
surface of the bone appears to have been convex both in length and
breadth. The size of the bone can only be inferred from comparison
with allied genera. From its imperfect condition I do not feel
assured that this bone may not belong to the larger species.
Right Scapula.
This comparatively small bone, though corresponding in a general
way with the larger specimens described (see fig. B, p. 656), presents
remarkable differences, which enforce the conviction that it belongs
to a very distinct species. The blade of the bone is flat, and presents
no curvature of plane; its anterior margin is relatively straighter ; the
acromion was smaller and differently placed, and approached almost
to the margin of the humeral articulation. As in the other species,
the surface for union with the coracoid is eroded, though apparently
to no great extent ; and though the bone is imperfect at the oppo-
site free end, there is no reason to suppose that it extended appre-
ciably beyond the part preserved. The extreme length of the spe-
662 PROF. H. G. SEELEY ON THE REPTILE
cimen is 184 centim. The length of the posterior margin to the
humeral articulation is about 15 centim., the length of the chord of
the arc of the posterior curvature is 134 centim., and the abscissa
is about 28 millim.; so that the curvature 1s much less than in the
large species. The posterior margin is also more inflated; it is
similarly sharp at its distal end; but the bone thickens steadily
towards the humeral end, where it rapidly expands, chiefly on the
inner side, to form the humeral articular surface. The posterior
margin is more rounded on the external than on the internal sur-
face, giving the effect of an obscure ridge along the visceral border
of this outline of the bone. The anterior border is also well rounded
and thicker than the posterior border, the thickness in the middle of
the blade being about 12 millim. The outline divides itself into a
proximal part, which is concave, and a distal part, which is straight.
The middle convexity of the outline is much less pronounced than in
the larger species. The concavity towards the proximal end is due
to the prolongation forward of the comparatively thin process for
union with the coracoid. The middle part of the anterior margin is
marked with fine parallel muscular ridges; and from this region
the spine of the scapula is prolonged downward obliquely across the
bone, so that it terminates at about the middle of the proximal end
of the bone, which is 9 centim. wide. The least width of the blade in
the middle of the concavity on the anterior side of the margin is less
than 5 centim. The width at the origin of the spine of the scapula
is about 53 millim.; and the width at the distal end, as preserved, is
63 centim. The spine is remarkably straight; and even the length
to its acromial termination is nearly 10 centim.; it does not so
much suggest the form of spine in a mammalian scapula as that of
Hatteria, existing as a broad rounded ridge, which divides the
proximal end of the external surface of the bone into two areas,
which are both concave in length, though the outer subtriangular
area is rather wider and shallower. The acromial process is imper-
tectly preserved proximally ; and hence the spine appears to termi-
nate in a rounded ridge which is about 2 centim. high and ap-
proaches to within a centim. and a half of the humeral articulation.
The thickness of the bone from the internal to the external surface
at the worn or eroded termination of the spine of the scapula is 4
centim. The width of the process is less than 14 centim.; and the
measurement from its outer border to the anterior coracoid margin
is about 5 centim., or over 4 centim. from its inner margin to the
posterior humeral articulation. The visceral surface is remarkably
flat; but beneath the region occupied by the spine the base was
somewhat concave. The humeral articular surface obliquely trun-
cates the inner half of the proximal end. Itis much roughened and
grooved with the marks of a cartilaginous epiphysis, and was broader
in proportion to its length than in the larger species. It shows
some sign of crushing, and is fully 4 centim. wide and 47 millim.
long. Its posterior outline is much broader than in the larger spe-
cies ; and the axis of the articular surface was not materially different
from the plane of the blade. The thickness of the anterior coracoid
FAUNA OF THE GOSAU FORMATION, 663
process was but little more than 15 centim. where widest, and became
somewhat narrower as it extended outward.
Humerus.
Both the mght and left humeri are strong bones (Pl. X XIX.
figs. 1-3) which, previously to fossilization, had lost both proximal
and distal articular ends. They are of exactly the same length as pre-
served, and are mutilated in almost the same manner, the distal ends
especially being obliquely truncated from behind forward; and they
show a subquadrate section. The right humerus is slightly the
more perfect ; and neither bone is distorted by pressure.
The fragments are 8 inches long; and, as preserved, the right
humerus is 47 inches wide at the proximal end ; the left humerusis
4 inches wide; the shaft is most constricted in the middle, where it
measures 1, inch from side to side; there is no corresponding con-
striction from back to front; but in this position the antero-pos-
terior measurement is 14 inch. The bone widens distally ; but, as
preserved, the distal measurement from side to side is only 2,3,
inches. The proximal articular head was nearly in the same plane
as the distal end. The inner lateral outline is gently concave;
the external outline is deeply concave, owing to the expansion out-
wards of the large thick deltoid process, which is bent at a consider-
able angle with the shaft. The antero-inferior and postero-superior
outlines are both nearly straight, though very slightly concave ; and
they converge slightly from behind forward, owing to the slight distal
twist giving to the bone an appearance of thickening to that end.
At the distal end the shaft becomes flattened both in front and
behind ; and these surfaces are nearly parallel; and, where fractured,
the bone is here 1,6 inch thick on the outer side, and somewhat
thinner on the inner side. The remainder of the inferior surface
is anterior to, and makes a slight angle with, the subtriangular
flattened distal area. It also may be said to be a long triangle ex-
tending from the inner corner of the distal articulation forward to
the divergent elements of the proximal end (fig. 2). Nearly its whole
length is straight ; and its middle portion is more rugose with mus-
cular attachments than the rest of the bone: the markings have the
appearance of slightly impressed ovate pits, which extend for a length
of nearly 3 inches. This inferior area is defined by faint lateral
ridges, and proximally, beyond the muscular markings, becomes
somewhat deeply concave from side to side, and compressed towards
the superior aspect, so that in length it is convex. This area is a
little inflated on the inner portion, and terminates laterally in a
slight sharp ridge. The outer expanded wing has a well-rounded
margin.
Superiorly the bone is highly convex from side to side (fig. 1),
though somewhat flattened on the inner and posterior side, and
also on the expanded external process, which is smooth and
slightly concave in length, and slightly convex from within outwards.
The upper aspect of the bone is divided into two portions by an
664 PROF. H. G. SEELEY ON THE REPTILE
oblique moderately elevated muscular ridge, which extends for about
32 inches across the middle of the shaft from near the inner side
proximally towards the outer side distally ; and though the whole
superior surface, except the expanded crest, is roughened with mus-
lar lines, another fainter ridge may be traced simane straight dis-
tally from the proximal termination of the oblique ridge. Imme-
diately below the proximal articulation in the middle of the shait is
an elevated muscular boss about 14, inch in diameter, which, as
preserved, is subcircular. The thickness of the shaft at its inner
margin is 1,5, inch, and at its outer margin 1-3, inch. The radial
crest hickeane towards the proximal surface, “and curves a little
upward. The outline of the fractured proximal end is somewhat
boat-shaped and compressed (fig. 3). This humerus is quite distinct
in character from any form of which I have any knowledge.
Femur.
The right femur (Pl. XXXI. fig. 5), found in 1876, is 10,2, inches
long. The left femur (Pl. TOOL fig. +), found in 1877, 18 hardly
more than 10 inches long. This difference i is apparently dns to the
different ways in which the bones are compressed. They are both
in the same state of mineralization, of a rich chocolate-brown colour,
and quite free from matrix, which has been removed by Professor
Suess. The bones belong to a somewhat distinct type; they offer many
resemblances, as Professor Suess pointed ‘out to me, to Cr yptosaurus
of the Oxford Clay, but are more slender. They therefore show the
typical characters of Dinosaurs, though there is a difference from
all English genera in the proximal anterior trochanter not being
separated from the shaft ; and there is a remarkable development of
muscular ridges on the bone, one of which extends on the proximal
posterior face (fig. 4)in a curve upward and outward from the small
middle trochanter on the inner margin of the shaft to the outer
and external margin of the proximal articulation. It is impossible
not to recognize the similarity of this strong muscular ridge to the
ridge seen on the corresponding aspect of the mammalian femur ;
and if this coincidence be admitted, it goes far to prove that the
middle trochanter, which is the most distinctive mark of the femur
of a Dinosaur, is homologous with the inner or lesser trochanter of
man; and so far it would seem rather to imply a foreshadowing
of a mammalian plan of muscle-arrangement. A similar muscular
attachment to this may be observed in Crocodiles above the middle
of the shaft. From it an intertrochanteric muscular ridge extends
to the position in which the proximal trochanter of Dinosaurs
is seen when it is developed. The shaft is most constricted in its
distal third, where there is a slight flexure bending the distal arti-
culation backward ; both articular ends appear to have been highly
cartilaginous, since they are marked with ramifying furrows and
occasional pits. As is usual with cartilaginous surfaces, the arti-
cular margin is sharply defined.
The proximal articular surface is best preserved in the right femur,
— -
FAUNA OF THE GOSAU FORMATION. 665
and, as usual, consists of a subcircular head (fig. 5), which is directed
inward and forward, and a narrower external area. The posterior
border of the articulation is nearly straight ; but the anterior out-
line is deeply excavated between the head of the bone and the
external trochanter. The globose head measures 1; inch from front
to back; and may be considered to be 15% inch from within outward;
but the entire length of the proximal articular surface was about
3,2; iach. The articular surface beyond the head contracts to less
than | inch from front to back, but widens again to fully 1,3, inch
at the border of the external trochanter; as in Cryptosaurus ewme-
rus, the narrower external part of the articulation is concave from
within outward, and does not extend so far proximally as the
convex head by half an inch. The length of the bone to the distal
border of the head on its inner margin is not more than 9 inches.
The anterior proximal trochanter (fig. 5) is about 13 inch long, and
convex in length: so that it dies away both distally and proximally,
where it merges in the articular surface. It is rough with oblique
muscular markings, and rounds into the flattened bnt slightly con-
vex external surface, which is also roughened, with a triangular area
of muscle-marking 25 inches long, which tapers distally. Below
this area the external side loses its flattened aspect, and becomes
rounded from front to back.
The proximal half of the shaft is considerably compressed from
above downward, and is flattened on both aspects: its width from
within outward in a line with the distal limit of the proximal tro-
chanter is about 24, inches, and just above the lateral inner trochanter
about 1,4 inch, while just below the lateral trochanter the width
is about 1,3, inch ; and there, as the shaft becomes narrower, it
grows more convex from side to side. The superior or anterior
aspect of the bone is marked with a strong longitudinal muscular
ridge, which originates towards the hinder part of the articular ball,
curves a little outward and then inward, and extends as nearly as
possible in the middle line of the shaft for a length of 65 inches;
it is moderately elevated, strongest proximally. and dies away where
a distal flattening of the bone gives an aspect of flexure to the lower
part of the shaft. There is also a second muscular ridge, which
originates at the same point, below the outer limit of the proximal
head, and, running obliquely inward, curves round the convex inner
side of the bone and becomes merged in the proximal limit of the
trochanter. Both these ridges are iess marked than in the larger
species.
The posterior aspect of the shaft(fig.4)is much more flattened. The
strong muscular ridge to which I have already referred as defining
an area homologous with the obturator-region of mammals, extends
distally for nearly 3 inches, and then curves more sharply inward
to merge in the inner trochanter. rom this ridge extend obliquely
inward, so as to cross each other, two series of narrow straight
linear muscular markings. Parallel to the sigmoid curve of the
proximal articular margin, and about a quarter of an inch below it,
is a line of about six or eight circular vascular perforations.
666 PROF. H. G. SEELEY ON THE REPTILE
The lateral trochanter is placed, as usual, at the angle between
the internal and posterior aspects’ of the bone (fig. 4). It is moderately
elevated, about 14 inch long, 6) inch wide proximally, and tapers
distally ; it is placed exactly midway between the proximal and
distal articular ends. Below the trochanter the section of the shaft
becomes subtriangular, being flattened on the internal aspect and
posteriorly, and rounded on the external and anterior aspect.
The distal articulation is chiefly noticeable for the inflated expan-
sion of the bone at the external margin, and for the relatively large
size of the condyles (fig. 4). The articular surface is 3 inches long in
the left femur, which has this region best preserved ; it is very mode-
rately convex from behind forward, and very slightly concave from
within outward, and rounds gently into the anterior surface of the
bone, where a concave natural impression divides the anterior
margin into a larger internal area and a smaller area which is
external. ‘There is the usual ill-defined gently concave pit for liga-
mentous attachment just above the articulation on the flattened in-
ternal surface of the bone, which looks obliquely upward, much as
in Cryptosaurus. The internal condyle is the larger of the two ; it
is about an inch wide, and curves round considerably on the paste
aspect of the bone, so as to cause the articulation to measure 2,2 To
inches is om front to back. The interspace between the condyles is
about ;% inch; and in this region the articulation measures, from
front to back, 1> inch. This depression becomes prolonged up the
middle of the posterior side of the shaft towards the inner part for
about 14 inch. The smaller condyle is more compressed, about
= inch wide, and gives an antero-posterior measurement to the arti-
cular end of 2 inches; and external to this condyle is a concave area or
eroove, + an inch wide, which defines it from the well-rounded broad
external margin. The small part of the articulation external to this
condyle makes a considerable angle with the major part of the sur-
face. The anterior® half of the articular surface is nearly smooth ;
but the posterior half is deeply scored with about eight comparatively
straight grooves, six of which lie between the condyles. These
grooves appear, from their corresponding development at the anterior
part of the proximal articulation, to be in the positions of greatest
pressure and greatest condylar growth, and may be regarded as evi-
dence that the bone was carried in an oblique position, as among
mammals.
Tibia.
A smaller pair of tibial bones are much less perfectly preserved
than those of the large species, only exhibiting about 6} inches of
the middle of the shaft (Pl. XXVII. fig. 19). Their ends are
decayed in the usual way; and distally the fractured outline was
subtriangular, but formed a triangle in which the anterior and two
converging posterior elements rounded into each other, and were
subequal. Here the extreme antero-posterior measurement 1s
about 1,2; inch, and the extreme width from side to side at the
distal end is the same. In the middle of the shaft the antero-posterior
FAUNA OF THE GOSAU FORMATION. 667
measurement remains unaltered, but the side-to-side measurement
is reduced to 42 inch; where the specimen is fractured proximally,
the antero-posterior measurement is $/ inch, while the measurement
from side to side in the middle of the shaft is 1,1, inch. The right
tibia (fig. 19) does not appear to be crushed ; but the left specimen
is somewhat fractured at its distal end. ‘The inner side in both is
flattened, though not quite so flat as in the larger species. The outer
side 1s convex, but divided into two portions by a median ridge,
which in its upper 34 inches is strongly muscular, though the
markings appear to be stronger on the left tibia than on the right—
a condition the reverse of that which obtains in the larger species.
The muscular ridge is made up of three or four close parallel ridges.
The posterior half of this side of the bone appears to be more flattened
than in the larger species, while the anterior half shows indications
of a similar longitudinal concavity, though the specimens are frac-
tured too low down for more than the beginning of it to be detected.
The proximal fracture displays a triangular outline with a long
straight base formed by the inner side and two shorter converging
sides which form the outer side. Here the bone is less than twice
as deep as it is wide. On the posterior side, as compared with the
larger species, the side-to-side compression is greater towards both
the proximal and distal ends, while anteriorly the bone is rather
more rounded from side toside. ‘There is about as much difference in
size between the two types of tibie as there is between the two kinds
of femora, though, so far as can be judged from the fragments
preserved, the differences in essential characters in the tibize were
less important than those of the femora.
There have also been found fragments of patelloid ridges of
tibiee which appear to belong to a species slightly larger than either
of these; but the materials are too imperfect for description, or even
for absolutely certain osteological identification.
Fibula.
The specimen which Bunzel (pl. i. f. 12, 138) regarded as the
upper half of the left humerus of a Crocodile is undoubtedly a
somewhat obscure fossil. It, however, presents nothing in common
with any crocodilian humerus with which I am acquainted, espe-
cially differing in its remarkable compression, in wanting all trace
of a radial crest, in the lateral compression of the shaft at right
angles to the supposed head of the bone, and in the inflation of
the inferior side of the head. While, therefore, [ have no hesitation
in affirming that the specimen is not crocodilian and not a humerus,
the loss of the terminal articular end and the evidence of a certain
amount of crushing makes any other determination a matter re-
quiring some caution. The contour, however, of the bone is so
similar to that of the tibia of Cratcwomus, and one aspect, and especi-
ally the posterior margin, is so roughened with muscular attach-
ments, that I have little hesitation in affirming that we have here
the fibula of one of the Dinosaurs—a view which is further sup-
668 PROF. H. G. SEELEY ON THE REPTILE
ported by the circumstance that the tibia has a strong ligamentous
ridge that would correspond to the rough side of the fibula.
Moreover I have found a further small portion of the supposed shaft,
not absolutely continuous, but showing that the bone retained the
same characters for some length further, and did not expand at its
distal end. It therefore may be well to state that this specimen
(Pl. XXVII. fig. 20) is to be regarded as a right fibula imperfect at
the proximal end, but, as preserved, 44 centim. wide. As pre-
served, the main piece of bone is over 10 centim. long, and, with the
additional fragment and the lost interspace, would indicate a length
of about 14 centim. The distal end is imperfect, having decomposed
before fossilization. The anterior margin is concave, the posterior
margin straight and rugose. The thickness of the proximal end, as
preserved, is about a centimetre, while the fractured distal end is
7 millim. thick and about 17 millim. wide. As remarked by Bunzel,
the distal fracture is semiovate, but the flattened side is towards the
transversely convex head of the bone, while the convex distal outline
is towards the transversely concave or external surface of the head.
Other fragments of similar character, also presumably fibular, but too
imperfect for detailed description, may be referred, one to a larger
and one to a smaller Dinosaur.
Metatarsal Bone.
(See Biinzel, pl. iv. figs. 11, 12.)
The specimen regarded by Biinzel (t. iv. f. 11, 12) as the phalange
of a Crocodile is almost too imperfect for accurate determination ;
but since it is certainly either the second or third metatarsal of a
Dinosaur, probably the former, it requires a shght notice. As pre-
served, it is little more than 64 centim. long and about 3 centim.
wide in front. What I take to be the inferior surface is the best
preserved ; only a small portion remains of the anterior articular
end, which was unusually convex from above downward. The lateral
outlines are concave; and the bone measures only 2 centim. from
side to side in the middle, where most constricted. ‘The superior
surface was compressed, so as to form an obscure broad rounded
ridge on the outer side, with a very shght broad channel below it on
the inner side. The depth of the bone in the middle of the shaft is
21 centim. The under surface is concave in length, flattened from
side to side, with a slight twist in the plane, which is directed a little
inward as it extends forward. The posterior fractured end is sub-
triangular, owing to the flattening of the base.
Claw-Phalange.
(See Bunzel, pl. iv. figs. 4, 5.)
A claw-phalange (Pl. XXIX. fig. 6), probably pertaining to the
second or third digit of the left hind limb, as indicated by Bunzel,
is ascribed by that writer to a species of Scelidosaurus, but may
be referred to Cratwomus lepidophorus. It is 33 millim. long, 25
millim. wide behind, and 22 millim. wide in front, is compressed
FAUNA OF THE GOSAU FORMATION. 669
from above downward, and, though blunt anteriorly, is most com-
pressed on the right border. The articular surface is imperfectly
preserved, but was concave from above downward, straight trans-
versely, and inclined obliquely to both superior and inferior aspects.
The superior surface, which is slightly convex from side to side,
is margined on each side by a strong groove, which is not very
deep, and extends forward for more than half the length of the
bone. Between these grooves are a number of slight parallel
ridges. At the sides the bone is excavated for the attachment of
powerful ligaments, more so on the left side than on the right; and
on the left side the irregular excavations extend further forward.
The under surface is comparatively flat, but concave in length, convex
from side to side, and marked in the middle with two irregular longi-
tudinal grooves,which have a tendency to branch as they pass forward.
These grooves are very imperfectly indicated in Biinzel’s figure, which
gives no indication of their dendroid character. The posterior outline
of the bone is ovate, and less than 2 centim. deep.
Dorsal Vertebra.
(See Bunzel, pl. 1. figs. 24, 25.)
A dorsal vertebra with the neural arch fairly well preserved is the
best vertebral evidence of this species(Pl. XXX. fig.5). The centrum is
4 centim. long, flattened on the under side, where it is 14 centim. broad
in the middle, where most constricted ; it is concave from front to
back. The sides are compressed and somewhat concavely excavated
below the neural arch, where the least transverse width is 1+ centim.
Thus the body of the vertebra in section would be subquadrate.
The anterior articular surface of the centrum is concave, 32 millim.
broad, and 27 millim. deep. ‘The posterior end is not concave, but
somewhat flattened and convex from above downward. The margin
is a little worn; the greatest transverse width is less than 3 centim.,
the greatest depth 25 centim. The neural arch is high, though not
unusually so for a Dinosaur. Its base is nearly as wide as the
anterior face of the centrum. It extends the whole length of the
centrum, and has the aspect of being compressed from side to side
below the transverse processes. The borders of the neural arch are
excavated (fig. 5), moderately in front, and more deeply behind, to
form the intervertebral passage for the nerves. The least length of
the neural arch from front to back, in the middle of the neural canal,
is 25 millim. The length from the anterior to the posterior zyga-
pophyses is about 54 centim.; and the upper border of those facets
is fully that height from the base of the centrum. The anterior
zygapophyses are directed upward, forward, and inward. ‘Their
external surface is rounded. There is a V-shaped notch between
them in front; and they form the anterior border of a transverse
cup-shaped depression in front of the neural spine, the hinder
borders of which cup are contributed to by the transverse pro-
cesses, which are directed upward and outward, and placed between
the zygapophyses in the middle region of the vertebra. The neural
670 PROF. H. G. SEELEY ON THE REPTILE
spine is narrow and short, and placed on the hinder half of the
neural arch; only its base is preserved. The posterior zygapophyses
are circular facets placed below and somewhat beyond its hinder
termination. They converge downward, but are separated by a broad
groove. The height of the vertebra to the base of the neural spine, as
preserved, is 6£centim. The extreme width over the posterior zyga-
pophyses is 24 centim. The width of the groove between them is
about 4 centim. ‘The side of the neural arch is of the usual cha-
racter, with ridges ascending from the anterior and posterior ends of
the arch which converge upward; and the posterior ridge, which is the
better marked, passes into the strong ridge which extends under the
base of the transverse process (broken away on the left side) The
area between these two lateral ridges, which is unusually deep and
narrow and ill-defined, appears to be the capitular articulation for
the rib. The space posterior to the lateral ridges is concavely ex-
cavated. The transverse process is broken off short. I infer this
to have been an early dorsal vertebra. The posterior convexity of
the centrum shows it to have been full-grown. This, no less than
the long narrow articulation at the side, and the other characters
of the neural arch described, show it to indicate a distinct species
from the vertebre referred to Cratcomus Pawlowitschit.
MEGALOSAURUS PANNONIENSIS, Seeley.
There are two teeth of a carnivorous Dinosaur (Pl. XX VIL. figs.
21-23) which present some resemblance to the teeth of Megalosaurus
and Lelaps, differing in no character of importance except size, the
fineness of the serrations, and shortness and breadth of the crown.
One specimen is a crown tolerably perfect, fractured just above the
base and before the commencement of the fang (fig. 21). The other
is the lower half of the crown of a somewhat larger but similar tooth.
The more perfect specimen is 21 millim. long, curved backwards,
quite straight, convex on both sides, though rather more so on the
inner side, and with the inflation towards the convex anterior margin
of the tooth. The posterior margin is relatively straight, but 1s con-
cave. he surface of the tooth is marked with microscopic longitu-
dinal wrinkling and faint parallel transverse lines of growth, only
to be detected by the way in which they reflect light. The posterior
margin throughout its length is marked with perfectly regular
transverse serrations, which extend along the tooth like a fringe.
Towards the extremity of the crown the serrations become slightly
shorter. On the anterior border (fig.22)the serrations are of a similar
character, but only reach down the tooth for 13 millimetres, becom-
ing smaller as they disappear. There are about forty-five of these
minute chisel-like serrations in all this margin. Where they ter-
minate, the tooth is just appreciably narrower and the anterior
margin is rounded, so that the transverse section (fig. 23) is exactly
the same asin Megalosawrus. The serrations of the posterior margin
are larger than those of the anterior margin ; so that there are only
about forty in the entire length of the tooth. The antero-posterior
FAUNA OF THE GOSAU FORMATION. 671
measurement is over a centimetre, and the thickness 6 millimetres.
There are no bones that I could refer to this species; and when
they are discovered the teeth may prove to belong to an animal as
different from Megalosaurus as is Leelups.
ORNITHOMERUS GRACILIS, Seeley.
The specimen figured by Bunzel, pl. vii. figs. 22, 23, and regarded
(p. 15) as the middle of the dorsal rib of a lizard, is the distal half of
the shaft of the femur of a remarkable new Dinosaurian. From the
circumstance that Biinzel has figured the external instead of the
internal aspect of the bone, it would have been difficult to make this
interpretation without examination of the specimen. The fragment
(Pl. XXVIII. figs. 6,7) is only 53 centim. long, has a nearly circular
shaft 13millim.in diameter at the proximal fracture, becoming a little
more compressed distally from above downwards and slightly more
expanded from side to side. The specimen shows no trace of the
distal articular end; but distally the bone is a little flattened on the
inferior and posterior surface, and slightly compressed towards the
outer border. There is a distal curve in the bone, rather more
marked, perhaps, than in the crocodilian femur. Towards the proxi-
mal end of the fragment the transverse fracture passes through a
longitudinal muscular pit, margined below by an elevated muscular
ridge, which is prolonged further distally than the muscular pit,
and appears to have terminated in a free process, though the ex-
tremity of this is broken away. ‘This is the internal trochanter of
the Dinosaurian femur (figs. 6, 7). What remains of the muscular
impression is about 12 millim. long and half a centimetre wide.
What remains of the sharp ridge bordering it is 17 millim. long.
I am not acquainted with any Dinosaur in which the femur has this
cylindrical bird-like form. ‘The shaft is formed of dense bone with
a large medullary cavity about 7 millimetres in diameter (fig. 7),
and has, at first sight, rather the aspect of the bone of a bird than
of a Dinosaur. Though the fragment is so imperfect, it is so cha-
racteristic that I have ventured to refer it to a new genus.
DoRATODON CARCHARIDENS (Bunzel).
The sculpturing of the outer surface of the jaw, no less than its
general form, would seem to have weighed with Biinzel in referring
the specimen represented in his plate 1. figs. 29-32 to the genus
Crocodilus. I find myself unable, however, to accept this generic
determination, partly because the teeth are such as indicate a dit-
ferent genus, and partly because I am led to refer the maxillary
bone represented in the same plate, figs. 5-5, to the same genus
and probably the same species as the lower jaw; and this shows,
though the fragment is very imperfect, characters which are not
met with in the genus Crocodilus. But whether its affinities
are stronger with Crocodiles or with Dinosaurs is a matter
far from easy to determine. The lower jaw consists of slender
rami, having a length, as preserved, of about 137 centim. with-
672 PROF. H. G SEELEY ON THE REPTILE
out reaching back to the articular region. The jaws converge
forward to the symphysis, where the contraction ceases, and there
is a slight anterior expansion before the lanceolate anterior termi-
nation. The greatest width of this slight expansion is 24 centim.;
and the width of the diverging rami at 10 or 11 centim. from
the anterior termination is over 5 centim.; thus the jaw is re-
markably pointed. The lateral contour of the alveolar margin
is convex from before backwards in the region of the symphysis and
concave in length behind the symphysis. The symphysis is 3 cen-
timetres long, and is made up in the anterior and inferior part by the
dentary bone, and in the posterior and superior part by the opercular
bone, which, on the alveolar aspect, forms half the symphysis, while
inferiorly it only constitutes the hinder fifth. In Crocodiles the oper-
cular bone does not enter.into the symphysis. The anterior part of
the jaw in the symphysial region is excavated in a spoon-shape,
owing to the remarkable and vertical elevation of the alveolar margin,
an elevation which appears to have relation to the straightness and
vertical position of the teeth ; so that the fangs could not have made an
angle with the crown. The whole inner side of the ramus is formed,
as in crocodiles, by the opercular bone, which, as Biinzel remarks,
is smooth and slightly rounded at its inferior and superior margins,
and extends back beyond the alveoli, only showing in its anterior
part two or three nutritive foramina. The external surface of the
bone is formed of the dentary element, except, it may be, towards
the hinder superior border, where a suture appears to indicate on
the inner side a coronoid bone. On the under surface the jaw is
flattened at the symphysis, but the flattened area rounds up an-
teriorly to the alveolar margin; but, where the rami begin to diverge,
there is a distinct sharp angle between the base of the jaw and its
side, and this ridge is prolonged backwards for a large part of the
region through which the teeth extend: and here the base of the
ramus is slightly convex from side to side till, with the fading of
the angle into the upper surface, it becomes more rounded and nar-
rower. ‘The suture for the opercular bone runs along the inner
third of the base. In ornament, the anterior expanded end of the
snout is pitted much after the pattern of crocodiles, and evidently
with similar relation to a vascular condition; but inferiorly the
ramus is marked with rough, short, irregular longitudinal ridges,
which extend round onto the side but do not risé to the alveolar
region, Which is comparatively smooth and marked with a row
of relatively large foramina, about seven’ or eight in number,
and placed above the middle of the lateral margin in a concave
line or groove. As they extend backwards they rise nearer to the
alveolar margin, and form the basis of a slight compression of the
bone above them. Posterior to the symphysis the depth of the
jaw increases: it is about 9 millim. in front, 17 millim. at the
last tooth- socket, and 3 centim. in the coronoid region; so that
it increases in depth more rapidly behind the teeth. It is
difficult to count the exact number of sockets; for some of
the fangs are preserved, and in other cases the teeth have fallen
FAUNA OF THE GOSAU FORMATION. 673
out: but there were not fewer than fifteen; and as the alveolar
groove is carried back and becomes very shallow beyond this
point, it is possible there may have been five teeth more, of small
size, in the hinder part of the jaw, making a total of twenty. The
teeth are largest in the middle of the jaw; but only the tenth on
the right side has the crown preserved in situ. The crown is 8 mil-
lim. high, and nearly 6 millim. wide at its base. It is trian-
gular in lateral outline, is curved inwards and directed upwards,
inwards, and backwards. Its base is rather less than 3 millim.
thick. Hach surface is convex, terminating in a sharp cutting-edge,
which is very finely serrated along the margin. In front and be-
hind there is a constriction, so as to separate the sides of the crown
from the elliptical fang; but this constriction is not appreciable on
the interior or the exterior aspect of the tooth. This form of tooth
is entirely Dinosaurian. Four teeth have been found separately
which show the same character. ‘Two of these are crowns broken
off directly from the fang, and show the constricted oval base of the
crown where the lateral ridges become pinched in. These teeth
are sharply pointed, and have the surface smooth to the naked eye.
There are also two teeth which have the same general form, except
that the crown is broader and shorter; and, owing to this circum-
stance, the serrations, which are transverse to the cutting-edge,
have an appearance of being directed obliquely upward. These,
however, are probably successional teeth, it may be from another
part of the jaw, or from the upper jaw. A certain amount of varia-
tion is obvious, because the fang of the eleventh tooth on the left
side shows that the base of the crown was marked with blunt
parallel ridges.
There is a fragment of the anterior end of a right dentary bone
from which the opercular element has come away, and which clearly
belongs to the same genus. It may indicate another and smaller
species, since the rami appear to diverge more rapidly, to have con-
tained more numerous teeth, with smaller and more circular fangs,
to want the anterior elevation of the jaw in its presymphysial region,
to be devoid of the ridge between the base of the jaw and the side,
and to have the side convexly inflated instead of flattened, especially
external to the alveolar margin. The ornament also appears to be
slightly different ; but as no teeth are preserved I have not thought
_ it necessary to give a name to this fragment. The length of the
dentary symphysis is 12 centimetre, and the length of the fragment
43 centimetres. The corresponding length of the dentary symphysis
in the larger specimen exceeds 23 centimetres.
The fragment of upper jaw briefly described by Biinzel, p. 6, pl.1.
figs. 3-5, I have, as already mentioned, identified with the lower
jaw of the large species just described. Notwithstanding the circum-
stance that Biinzel remarks on its close resemblance to existing
erocodiles, he places the nasal aperture immediately in front of the
orbit, which alone would suffice to show that the type differed from
crocodiles fundamentally. In fact, the perforation of orbit and
nares in the maxillary bone would be a modification of old-fashioned
Q.J.G.8. No. 148. : 2¥
674. PROF. H. G. SEELEY ON THE REPTILE
anatomy of no ordinary kind, since the maxillary bone does not
enter into either the orbit or the anterior nares of the crocodile, and
it certainly does not enter in any known Dinosaur into the external
wall of either of these vacuities. Agreeing with Biinzel, that the
margin which he regards as the anterior border of the orbit is cor-
rectly identified, I regard the perforation which he terms nasal as
the preorbital vacuity characteristic of Teleosaurs, and more or less
developed in various Dinosaurs. The bone between the orbit and
the preorbital vacuity is always the lachrymal; and I therefore
identify the lachrymal bone as united by suture with the maxil-
lary. The length of its base is 2 centim.; but it is fractured
superiorly, and therefore its outline cannot be stated, further than
that it appears to have been triangular. The posterior margin
is concave, rounded and thickened, with an indication of a groove,
which may have had relation to the lachrymal canal. The surface
is sculptured with somewhat oblique ridges, which are short and
irregular, and deeper than the sculpturing on the maxillary. The
suture with the maxillary is straight but slightly oblique, so that it
laps a little further down on the inner than on the external surface.
The preorbital vacuity only shows a small portion of its basal
margin, which is rounded. The lachrymal bone in front of it is
thin, and gives the aspect of the vacuity having penetrated ob-
liquely inwards and forwards. A small portion is preserved of a
suture on the superior surface, which is straight and parallel to the
alveolar surface, or but slightly inclined forwards. Hence it may
reasonably be identified as the suture for the nasal bone. The
depth of the bone from the nasal suture to the alveolar border
is 22 millim. Anteriorly the bone is fractured, so that there is no
indication either of its length or of the length of the nasal suture,
or of the nature of its relation to the premaxillary bone. ‘The pos-
terior end is also fractured ; but just below the orbital border there
is a minute indication of a suture, evidently indicating the malar
bone, and showing that its relations were the same as in Dinosaurs.
The surface of the maxillary bone is marked with an indefinite
rough sculpturing, which, in the upper part, has a tendency to
assume a linear character; and the hinder part is somewhat lightly
pitted. The internal surface is necessarily irregular ; and its appear-
ances may be passed over in so far as they relate to the region
above the palate ; but above the alyeoli the bone evidently developed
a horizontal palatal plate, which has been almost entirely broken
away. It appears to have been notched out posteriorly into a post-
maxillary vacuity, such as is seen in the crocodile, since the hinder-
most 14 centimetre is a smooth, sharp, somewhat concave margin
bordering the alveoli.
It is very difficult to understand the alveolar structure from an
inspection of Biinzel’s plate, since it gives the appearance of a double
row of tooth-sockets: this is due to the circumstance that while the
tooth-sockets (in which most of the teeth still remain) are placed
close to the outermost alveolar border, there is, internal to them, a
parallel series of pits which are broad and shallow, and are, I think,
FAUNA OF THE GOSAU FORMATION. 675
produced by the circumstance that the teeth of the lower jaw were
received scissor-like between the teeth of the upper Jaw; and these
pits I regard as excavations which have resulted from the pressure
of their crowns—a view which is especially supported by the cir-
cumstance that they are deeper posteriorly, where the palatal border
is but little above the outer alveolar border, and are less marked
anteriorly, where the palatal border rises about 8 millim. above
the alveolar border. The teeth extend along the whole alveolar
length, which is 44 centim., and were eight in number in the
fragment. ‘They are larger in front than behind, and mostly ap-
pear to have been successional teeth not fully cut. The first,
where broken, is 7 millim. long and 4 millim. thick. The second
is less than 4 millim. long, and is clearly a section of the fang;
but one of the later teeth shows the sharp serrated cutting-edge,
compressed form, and smooth enamel characteristic of the teeth of
the lower jaw; and it is on this evidence that I have felt justified
in referring it to the same species. Both fang and crown appear
to have been hollow ; but as the cavities are filled with iron pyrites,
I have not been able to excavate them.
There are a few other unimportant fragments, chiefly of the lower
jaw, which exhibit similar sculpture, and presumably belong to this
genus, but too imperfect to be worthy of description.
There is a small claw-phalange (Pl. XXVII. fig. 26) which,
perhaps, for the present may be noticed here, seeing that it is quite
impossible to say with certainty to which of the animals it belonged.
It is 17 millim. long, curved downward and to the right. It tapers
to a point, and is subtriangular, being flattened on the under side,
on the left side, and obliquely on the right side, which is large.
But these three surfaces round into each other, except where they
are divided by the sharp lateral ridges which margin the base. The
articulation is 7 millim. deep, a little narrower, concave from above
downwards, and convex from side to side.
RHADINOSAURUS ALCIMUS, Seeley.
I found this genus upon the femora, which are quite distinct from
any thing hitherto discovered. The humeri are such as would be
associated with those bones, though there is no proof beyond simi-
larity of character that they belong to the same species. The same
remark applies to the vertebra, which are such as might be expected
in an animal of this kind; but there is no evidence of natural asso-
ciation. I have placed this genus next in succession to Doratodon,
because that genus is founded upon a head, while this is formed for
limb-bones ; and though there is no evidence to justify their bemg
thrown together, there is a possibility that Doratodon belongs to
one of the animals of which the head cannot be identified.
Humerus.
Two specimens of humeral bones (Pl. XXXI. figs. 8-10) exhibit
characters indicative of an animal in many respects unlike any other
2y 2
676 PROF. H. G. SEELEY ON THE REPTILE
in the deposit, especially in the slenderness of the shaft and relatively
small size of the articular ends, as well as in the circumstance that
the articular extremities were at right angles to each other. Unfor-
tunately both proximal and distal ends are lost by decomposition.
The left humerus is best preserved proximally, while the right .
humerus extends further distally. The length indicated by the two
bones without reaching the articular ends is 14 centim.; so that
the entire length of the bone, when perfect, was at least 2 centim.
more. The left fragment (fig. 8) is fully 12 centim. long, and, when
placed with the distal end uppermost, shows a slight convexity on
one lateral margin and a corresponding concavity on the other,
the concavity facing the anterior and inferior aspect of the bone,
the convexity being superior. Owing to the circumstance that the
proximal end is absolutely at right angles to the distal end, it hap-
pens that the shaft of the kone widens distally. The transverse
measurement at the base of the radial crest (fig. 9) is 14 centim., and
atthe distal fracture 23 millim. (fig. 10); and it is still widening.
The superior distal surface is convex from side to side, with a slight
ridge towards the radial side of the bone, which is really a prelon-
gation of the muscular ridge of the radial crest, which in crocodiles
never extends along the superior aspect of the bone. This ridge
produces a flattened radial aspect, a slight approximation to which
may be observed at the distal articular end of the crocodilian hu-
merus ; but here it gives a somewhat compressed and sharp aspect
to the inferior radial margin of the bone along the distal half of the
shaft, while the ulnar side is relatively flattened or rounded. The
bone is marked, on the superior aspect especially, with strong longi-
tudinal strie or slightly elevated ridges. _ Its thickness at the distal
end, as preserved, is about 13 millim. ; but the right bone is a
trifle stouter. The inferior aspect is flattened distally with a slight
longitudinal depression. The proximal end of the bone necessarily
widens, while the shaft remains comparatively uniform. The su-
perior surface is smooth, and convex from side to side, but slightly
channelled towards the expanded radial process, which is necessa-
rily placed on the middle of the aspect which, when viewing the
distal end, would be regarded as superior. The width of the
proximal end appears to have been small. The lower part of the
_ radial crest gives a transverse width, as preserved, of less than
21 centim. The inferior aspect of the proximal end ‘is longitu-
dinally channelled, and thus divided into a compressed anterior
process and a rounded and somewhat inflated inferior and posterior
part. The thickness of the bone here at the fracture is just over a
centimetre. The whole inferior surface, not only of the radial crest
but of the adjacent region of the bone, is roughened with powerful
muscular attachments. The right fragment substantially repeats
these characters; only the bone is appreciably stronger, with its
muscular ridges more marked, and in length shows a decided sig-
moid curve, like that which marks the humerus of a crocodile. I
am led to refer these bones to the same species as is indicated by
the femora next described. In this case they would indicate an
Low
FAUNA OF THE GOSAU FORMATION. 677
animal with remarkably small anterior limbs, suggesting the pro-
portions of a Teleosaur. I may state that this identification is
founded chiefly on similarity of general aspect, superficial texture,
condition of preservation, and colour.
Femur.
(See Biinzel, pl. ui. fig. 1.)
A pair of remarkable slender bones, somewhat crushed, and with-
out trace of an articular end, which, at first sight, have the aspect
of being portions of ribs, I am disposed to regard as the femora of
a small Dinosaur, having probably Teleosaurian affinities. Yet such
an identification is necessarily somewhat conjectural; and I would
therefore state that | am led to the conclusion that the bones are
femora (Pl. XXXI. figs. 6,7) by their slightly curved form, by
the widening of what I take to be the proximal end, by the
slightly smaller size of what would be the distal end, but chiefly
by a large somewhat oblique muscular scar with an elevated border
in its lower part, which is situate in the same position as the
middle trochanter on the femur of a Dinosaur, which also looks
inwards, backwards, and downwards. And I do not recognize so
many probabilities in favour of any other interpretation, especially
as only two bones have been found, which are right and left,
while nearly all the other limb-bones are similarly represented
by pairs. The longer specimen measures about 6 inches; it is
1-3, inch wide proximally ; ; and the trochanteroid scar reaches to
within 13 inch of the proximal end. At its upper ne the bone is
1% inch ae The scar is 1,5 inch long,
in its greatest width in the middle (fig. 6). It causes the son
to swell out in thickness, so that the internal border is much
thicker than the external border, which appears to be somewhat
compressed, and which is slightly convex in length; while the inner
border of the bone, but for the trochanteroid bulge in its lower
part, would be slightly concave. As it is, it is divided into two con-
cavities. ‘The widening of the bone at the proximal end I take to
indicate the base of the proximal articulation. The specimen is
there slightly incrusted with pyrites; but no trace is preserved of
either articular head or external trochanter. The long oval of the
lateral trochanter is defined by a ring, which is slightly elevated in
its proximal and internal part, and much more elevated on its distal
and anterior portion, which gives a width to the bone of 1,3, inch,
while the width at the distal end is $f inch. The thickness of the
bone at the distal end may be slightly diminished by accidental
compression. It is $4 inch on the inner side, which is less than
the thickness at the proximal end (fig. 7), where, in a corresponding
position, the bone measures 43 inch. The inner border, both proxi-
mally and distally, is convexly rounded ; the external border appears
to be flattened obliquely externally in the distal half, and com-
pressed and rounded proximally. But as the specimen is crushed,
this point remains obscure. These femora are among the most re-
markable bones that the Gosau formation has yielded.
678 PROF. H. G. SEELEY ON THE REPTILE
Dorsal Vertebra.
There are two dorsal vertebree, both a little crushed and without
the neural arches, which belong to such a Dinosaur. From the
more perfect of these I draw the following characters. The cen-
trum is 44 centim. long, with the articular ends flat, and about
2+ centim. wide. The anterior face appears to be rather the
flatter and larger ; but both articular margins are a little injured by
fracture. Their edges are defined by a narrow bevelled area; the
body of the centrum is smooth, regularly constricted, so as to be
concave from back to front in every position below the neural arch,
and devoid of ridges. It is more constricted at the base of the
neural arch than elsewhere, and, except in being much more slender
and less deep, recalls the dorsal vertebra of Anoplosaurus. The
neural canal is similarly narrow.
OLIGOSAURUS ADELUS, Seeley.
(See Biinzel, pl. vi. figs. 14, 15, pl. vu. figs. 1-4.)
The bone which Binzel figures (pl. vi. figs. 14, 15) and regards as.
the right humerus of a lizard, I regard as the right scapula probably of
a Dinosaur; while the specimens (pl. vii. figs. 1, 2, and 3, 4) regarded
as right femur and fragment of humerus of lizard, I regard, from
their correspondence in character and size, as probably referable
to the same animal, though the femur entirely wants the tro-
chanter which is usually seen in Dinosaurs. Taken by themselves,
these two bones have enough in common with lizards to account for
Biinzel’s determination ; but if the scapula is rightly associated with
them, there can, I think, be no doubt concerning their Dinosaurian
affinities.
Scapula.
The scapula is a slender compressed bone 44 centim. long, and
imperfect at both ends, but not so much injured as materially to
affect its characters. The inner or visceral side is slightly concave
in length, and makes no approximation to the concave form the
bone has in the crocodile. This inner surface is gently convex from
side to side. The posterior margin is nearly straight, becoming
slightly concave towards the proximal end. In adopting this no-
menclature I have followed the crocodilian analogies rather than
those of certain Dinosaurs. This posterior margin, as preserved, is
33 millim. long; it is rounded, rather compressed towards the free
end, and somewhat obliquely flattened towards the proximal end,
where a slight ridge becomes developed, which extends towards the
articulation, giving the bone a thickness of about 3 centim. The blade
of the scapula is moderately concave on its anterior border, which,
as preserved, is 3 centim. long. The width of the distal end is
11 or 12 millim; in the middle the blade becomes constricted to a
width of 1 centim., and then expands proximally. The proximal
width cannot be given, on account of fracture; but the specimen, as
preserved, is 17 millim. wide. The anterior margin is more com-
FAUNA OF THE GOSAU FORMATION. 679
pressed than the posterior margin. There is an indication of a ridge
towards the proximal end, similar to that on the opposite side of
the bone; and between these ridges, which are 13 millim. apart,
the proximal end of the bone is concave from side to side. The bone
does not greatly thicken at the proximal end, the greatest thickness
towards the anterior border is 6 millim. There is a general re-
semblance in character to the scapula attributed by Professor Owen
to Iguanodon Mantelli (Pal. Soc. 1854, pl. xiv. fig. 1); but in this
form the blade is not so constricted, and it may be doubted whether
the anterior process there so marked attained any corresponding de-
velopment in this fossil; nor is the resemblance closer to Scelido-
saurus; and, indeed, in the straightness of its posterior margin the
bone rather suggests the scapula of an Ichthyosawrus, in which, how-
ever, the straight margin is anterior.
Humerus.
The bone which Biinzel identifies as belonging to the right side
of the body seems to me to be referable to the left side. The
reason for this determination is that the articular head of the bone
is on the right side, as proved by the thickening, and the radial
crest on the left side. Like most of the other specimens, this is im-
perfect at both the articular ends, though enough remains to convey
an idea of the form and length of the bone before it was mutilated.
The shaft, which is greatly expanded proximally, is 5 centim. long.
The distal end has the superior and inferior surfaces parallel; and
the bone is 8 millim. thick and nearly 12 millim. wide, more
rounded on the anterior than on the posterior border. From the
superior outer border a faint rounded ridge extends up the shaft
towards the middle of the articular head; and an impression occurs
in its upper half which appears to be muscular. The width of the
bone at the proximal end, just above this ridge, is 22 millim. In-
ternal to the ridge the bone is compressed, so as to contribute to
form the articular head. External to the ridge it is transversely
expanded, somewhat flattened, and marked with strong longitudinal
srooves at the outer extremity of the radial border. The radial
border is more concave than the ulnar border. The thickness of the
radial expansion is about 6 millim., but diminishes proximally.
The thickness of the base of the proximal articulation where frac-
tured is about 9 millim. The inferior surface is regularly concave
from side to side at the proximal end, and convex in length, cor-
responding to the transverse convexity and longitudinal concavity
of the superior surface. The shaft where most constricted, in its
lower third, is less than 1 centim. wide, while its thickness steadily
diminishes from the distal end to the radial margin at the proximal
end. This bone possesses none of the typical characters of a lizard-
humerus, but all those which are usually found in Dinosaurs, though
I am unable to name any genus in which the form of this bone is
so closely paralleled as to suggest generic identity or even affinity.
The distal fracture, which is transverse, is so irregular as to suggest
an epiphysial surface from which the epiphysis has come away.
680 PROF, H. G. SEELEY ON THE REPTILE
Femur.
Biinzel, though referring this specimen to the right side of tne
body, has given no indication as to its proximal and distal ends.
These determinations are a matter of some difficulty; but it is well
known that, asa rule, a Dinosaurian femur is thicker on the inner
than on the external margin, which is commonly compressed: and
there is usually a certain compression of the bone on the posterior
surface. I have hence been led to regard this specimen as probably
the shaft of a left femur which has lost both the proximal and distal
ends. The fragment is 6 centim. long; the shaft is curved more
after the crocodilian than the Dinosaurian pattern; only it is a
simple convex curve, without any trace of a sigmoid flexure. The
shaft is nearly cylindrical, 1 centim. in diameter in the middle,
where most constricted ; and there it is about 9 millim. thick. What
I take to be the distal end expands transversely to 13 millim., is
flattened on the superior and inner borders, flat or concave on the
inferior border, somewhat compressed towards the external side.
The bone is 9 millim. thick on the inner margin, and 6 millim.
thick on the outer margin.. Proximally there is a nearly similar ex-
pansion of the bone; only the inner border is directed well inwards,
the external border is more flattened, and the inferior surface is
flattened. The width of the proximal end, as preserved, is 13 centim.
It is impossible, in the absence of more distinctive characters, to
form any opinion as to the affinities of this specimen. A curious
circumstance concerning it is that, while indubitably a left femur,
either end could be regarded as proximal.
Vertebre.
Two vertebre are figured by Biinzel, pl. vii. figs. 2-4, which he
regarded as indicating a foetal Dinosaur. It is difficult to discover
any evidences that would enable one to confirm this remarkable
speculation. The vertebre are beyond all doubt Dinosaurian; but
except in the fact that the neural arch is lost, there is no sign of
immaturity. The articular ends are perfectly ossified and almost
flat; and though the specimens are a trifle worn from rolling, 1 have
no doubt that they must be referred to a fairly well-developed
animal. ‘The larger and better-preserved vertebra has the centrum
14 centim. long, with the sides somewhat converging, but well
rounded below. There is the base of a transverse process, seen in
the middle of the side, just below the pit for the neural arch. This
circumstance determines the vertebra as an early caudal. The
transverse measurement over the bases of these processes is 14 millim.
The anterior articular surface is nearly circular, 13 centim. deep,
and nearly as wide, with the margin rounded and the articular sur-
face nearly flat. The posterior articular end appears to have been
rather small and rather more concave. The neural arch did not
extend the whole length of the centrum. The neural canal is con-
cave from front to back. There are no signs of facets for chevron
bones.
ee
FAUNA OF THE GOSAU FORMATION. 681
The second vertebra is about 1} centim. long, but had a keel on
the base of the centrum. It appears to have been smaller than the
other ; but, as the dorsal half of the centrum is not preserved, it may
be that this is a similar caudal vertebra.
There is no evidence that these vertebre belong to the animal
which possessed the limb-bones; and I have noticed them here be-
cause they are not obviously referable to any of the other species
described.
HopiosavRvs IscHyrvs, Seeley.
In June 1880 I received word from Prof. Suess that another
collection of Cretaceous reptile remains from the Gosau beds existed,
which was discovered long before the publication of Dr. Biinzel’s
paper. Eventually this small series was secured by Prof. Suess,
and forwarded to me. ‘The specimens are imbedded in a hard
calcareous clay, and are in a bad state of preservation, having
been fractured in the contortion of the rocks to an extent that
often makes identification of the fragments.extremely difficult.
Prof. Suess remarks of the collection, “It is not very much—a few
broken articular ends of limbs, a number of those thick roof-shaped
dermal plates well known to you, and a few fragments of vertebree—
the whole imbedded in a number of hard fragments of calcareous
clay evidently once united together, and clearly belonging to the
same individual; so they may be of some interest as showing to
which limb-bones the dermal plates belong.” They are certainly
the most unpromising set of fragments that I ever examined with a
view to the study of a new type of life; and yet they certainly in-
dicate a different species from any of which the other collections give
evidence. I have removed the matrix, and offer a few notes on some
of the more characteristic fragments. ;
Proximal end of right Humerus.
This fragment indicates a humerus very different from any thing
with which I am acquainted, but perhaps makes a near approxima-
tion to that reptilian humerus described by Mr. Hulke as probably
referable to Hylwosawrus. It has lost the radial crest, which appears
to have been reflected downward more conspicuously than in Mr.
Hulke’s specimen, and to have presented more of the Crocodilian
conformation, though it extended up to the articular head of the bone,
as is usual in Dinosaurs. The superior surface has been fractured,
so that the entire thickness of the humeral articulation is not de-
monstrated ; but it was evidently oblong, and measures 63 centim. in
width, and, as preserved, is 4 centim. thick just intermal to the
radial crest, and over 3 centim. thick above the ulnar tuberosity.
It appears to have been comparatively flat, and is remarkably pitted
with the evidences of a cartilaginous epiphysis. It appears to be
inclined at a considerable angle towards the radial side of the bone.
Towards the ulnar side it is rounded. On the ulnar margin it is con-
stricted ; and a portion of a tuberosity remains on the inferior sur-
face which is 2 or 3 centim. below the articular head, and increases
682 PROF. H. G, SEELEY ON THE REPTILE
the transverse width of the bone to about 8 centim., thus giving to
the head of the bone a blunt wedge-shaped aspect ; a concavity com-
pletely separates the tuberosity on the inferior surface from the
articular head. Unfortunately I have not found it possible to clear
away the matrix from the inferior surface, except so far as was
necessary to show that there was a concavity behind the radial crest.
The radial side of the bone is flattened, but a little concave from side
to side on its external aspect. It forms a considerable angle with
the superior face of the bone, from which it is divided by the ridge
or tuberosity which formed the ball-like part of the articulation ;
though this ball is fractured, it was placed conspicuously towards
the radial side; and beyond it is a longitudinal concavity.. The
fragment is only about 74 centim. long, and the fracture is not sharp;
but it shows that the shaft was becoming remarkably flattened and
compressed, especially towards the ulnar side.
The specimen thus presents a very marked difference from the
humerus of Anoplosaurus, and is unlike that of any other genus,
especially in the constriction which defines the ulnar tuberosity and
in the angle which it makes with the head of the bone.
There is a small fragment which might well be a part of the
middle of the shaft of this specimen, too imperfect for description ;
but if it really pertained to this bone, it may be interesting as show-
ing a thickness of nearly 23 centim.
A third fragment, very imperfectly preserved, I am disposed to
regard as the distal end of the right humerus, though it is so imper-
fect that I cannot speak confidently on the matter. It only shows
one condyle, which is almost globular, with the flattened lateral
margin of the bone and a small adjacent part of the superior surface
of the shaft. This condyle, however, is remarkably massive, is
rounded, less than 4 centim. thick, and 43 centim. wide, with a
rugous articular surface extending internally parallel to the external
lateral surface of the bone, and indicating, if I have correctly guessed
the nature of the fragment, that the ulna developed a process received
between the condyles in an unusual manner. The bone was evidently
concave from side to side in front and greatly compressed between
the condyles, very much as Mr: Hulke has represented in Hylco-
saurus; it was thick on the ulnar side, and evidently more com-
pressed on the radial side.
Articular ends of Scapule.
The scapule are fractured so that the entire blade of the bone is
lost as well as the articular surface for the coracoid ; so that nothing
remains but the articular region. The left scapula is rather more
perfect than the right. The specimens have, at first sight, rather
the appearance of articular ends of caudal vertebre than of scapulee.
The left specimen shows the articulation to have been an elongate
ovoid with the internal margin of the articulation convex and the
external margin more flattened. The extreme width is 43 centim.,
and the length about 63 centim., as preserved. The articular sur-
FAUNA OF THE GOSAU FORMATION. 683
face was moderately rough, with the margin slightly rounded; and
it was concave from front to back. Just above the posterior rounded
termination of the articulation the bone is thickened so as to form a
very slight tuberosity, most conspicuous on the internal surface,
where a groove divides it from the articular head. This inferior
surface of the bone is convex from side to side, but soon becomes
compressed, so that the blade, where fractured, at 4 centim. from the
articulation, is less than 2 centim. thick. On the external surface
the specimen is concave above the articulation, partly because there
is a Slight rounded ridge on the posterior edge, not, however, separable
from the rounded posterior border, and partly because the bone is
becoming thickened anteriorly, evidently in relation to the develop-
ment of a strong spine or crest at about 2 or 3 centim. above the
articular surface. The articular margin is marked with longitudinal
lines of ligamentous attachment. It is of course impossible to speak
of the affinities presented by this form of scapula; but the bone ap-
pears to me to be distinct from the scapula of Cratcwomus, Anoplo-
saurus, Iguanodon, Scelidosaurus, and other types with which it
might be supposed to be allied.
A flat expanded bone, very imperfectly preserved, appears to be
a portion of a coracoid. It has but one margin remaining, which is
straight for a length of upwards of 5 centim. and indicates an arti-
cular surface at right angles to the bone, such as may have adjoined
the scapula. The specimen is upwards of 7 centim. broad and
10 centim. wide, as preserved, but is too imperfect for description.
Vertebre.
The vertebral fragments have shared in the general fracturing.
There are two portions of sacrum which had thoroughly decomposed
before fossilization. One fragment indicates two vertebree anky-
losed together; the other fragment I regard as showing the base of
the centrum of another vertebra, and on this evidence should infer
that there were at least three, and probably four, sacral vertebree,
though the second specimen is imperfect in every direction, so that
it has to be regarded carefully to be accepted as a vertebra at
all. This fragment, as preserved, is 5 centim. long, broad, rounded
on the under side and somewhat flattened, with a shallow median
depression which is fully 1 centim. wide.
The same characters are shown in one of the ankylosed vertebre.
These also are imperfect at both ends, so that it is impossible to judge
what the length of each centrum may have been; but, as preserved,
the length of the two together is a little over 5 centim.; and 3 centim.
of this belong to what I regard as the more anterior of the two. This
vertebra is very slightly concave from front to back, and convex from
side to side, with the aspect of being flattened on the under side and
with a very slight median depression, which becomes more marked in
the second vertebra. ‘The sides are rounded and concavely impressed
between the transverse processes. This appears to have been given
off at the suture between the two vertebre, which is somewhat ele-
684 PROF, H. G. SEELEY ON THE REPTILE
vated and expands laterally—though, from the fractured state of the
specimen, it is impossible to state the width across the vertebra,
which, as preserved, is only 5 centim., but may perhaps have been —
somewhat more. The centrum appears to have been depressed, as
usual in the sacral region, but there is no fracture showing its exact
thickness. This form of vertebra is very different from that referred
to Iguanodon by Prof. Owen (Pal. Soc. 1854, pl. 3), in which the base
of the centrum is a sharp ridge. It is also unlike, but nearer to, the
centrum represented by the same author, pl.7, and referred to a young
Iguanodon, in which the base of the centrum is flat, with a sharp
ridge margining each side.
There are two vertebre which appear to be caudal—one from
the early part of the tail, the other from the later part of the tail.
Both appear to have been equally long; and both are crushed. The
earlier caudal vertebra, as preserved, has the centrum about 45 centim.
long, and 22 millim. wide in the middle of the base. The anterior
face appears to have been concave, and, as preserved, is 43 centim.
deep; the depth of the posterior end of the bone is somewhat less.
The base is flattened, though concave in length, and separated from
the sides by a sharp angular ridge. The sides of the bone are con-
cave. ‘The transverse process appears to have been placed on the
hinder part of the centrum, below the neural arch, and to have had
an antero-posterior extent of no more than 17 millim. The neural
arch is compressed from side to side and constricted from back to
front, with a rounded ridge margining the straight outer border of
the neural arch, which is inclined obliquely backward. The zyga-
pophyses are imperfectly preserved. The posterior zygapophyses
extend beyond the centrum ; of the anterior zygapophyses no trace 1s
preserved. The later caudal vertebra has a constricted dicebox-like
form. Its contour appears to have been five-sided at the articular
ends, with a median ridge on the base and lateral ridges at the middle
of the sides. The length of the centrum is about 5 centim. Its
depth appears to be about 3 centim., and its width 34 centim. This
I take to be at the posterior end of the bone. Only an indication
of the neural arch is preserved ; the width of the canal increases pos-
teriorly as usual. Another vertebra, apparently dorsal, is imbedded
in the matrix ; but I have not felt justified i in excavating it so as fully
to display its characteristics.
Dermal Armour.
The dermal armour comprises plates of two patterns :—first, more
or less circular plates of moderate thickness; and angular plates
which are thick at one margin, thin at the opposite margin, and have
the surface concave in one direction and convex in the other. They
are flat on the under side. One or two of the small biscuit-like
plates present that curious angular combination of fibres that is cha-
racteristic of the armour referred to Hyleosawrus, a character which
rather suggests the etched surface of a meteorite than the structure
of ivory. I have been led to think that this armour of Hyleosaurian
FAUNA OF THE GOSAU FORMATION. 685
character is probably abdominal, or at least was not placed in a po-
sition so exposed on the-sides of the body as the larger and thicker
scutes. One of the plates, as preserved, is 6 centim. “long, less than
5 centim. wide, has the margin rounded, and not more than 3 centim.
thick (Pl. ROX L fig. 11). It shows the fibres crossing somewhat
obliquely, so as to define slightly rhombic areas. This structure is
suggestive of the transverse crossing of the fibres in ivory; but I
have no evidence whether it extends into the substance of the bone.
Another plate of about the same size appears to be rather
thicker, and, though retaining traces of the cross angular mark-
ings, has the surface of the scute a good deal pitted and marked in
lines with fine vascular perforations. The larger scutes appear to
have lost the cross striping and to show a more porous texture.
They are remarkable for having the angle on the scute placed so
near towards one margin as sometimes to make that side all but ver-
tical to the base. The other side covers nearly the whole superior
surface of the scute, and presents the curious saddle-shaped form to
which attention has already been drawn. One of these scutes is
63 centim. long, and has the angular crest 23 centim. high, while
the average thickness of the plate is not much over 1 centim. In
another specimen the crest appears to rise considerably higher, and
gives evidence of median compression and oblique overlapping ; the
base is slightly concave.
Besides these remains there are portions of ribs, which are slender,
Straight, flattened, or slightly grooved on one side and convex on the
other, with the anterior margin of the bone rounded and the posterior
margin compressed to a sharp ridge. ‘These fragments are all short
enough to appear straight, and have a width of about 13 centim.
There are a few fragments which give some information about the
characters of the articular ends of some of the larger limb-bones ; but
they are so obscure that I have not felt justified in attempting to
describe them; and there is a fragment which may be a portion of
an ilium, of unusual shape.
CrocoDILus PRoAvus, Seeley.
The remains of a proccelous Crocodile, some of which were figured
by Biinzel (pl. i.) comprise 2 cervical vertebrae, 8 dorsal, one lumbar,
one sacral, an early and a late caudal, portions of two iliac bones
(which unfortunately exhibit no characters of value), the proximal
end of a femur showing the typical Crocodilian characters in a very
pronounced manner, a the ulna and radius. There are Crocodilian
teeth which have lateral ridges and striated crowns, and small suc-
cessional teeth, and a renwal bone.
There is also evidence of a minute Crocodile in the articular head
of a femur. The fragment is too small for description; but it
obviously indicates a distinct species from the larger remains, as
shown by the greater forward curvature of the head, its relatively
greater width, atid the stronger development of the saath crest on
ihe under fide of the anverles surface.
686 PROF. H. G. SEELEY ON THE REPTILE
Femur.
The proximal fragment of the femur (Pl. XXIX. figs. 7, 8),
which may have belonged to the same animal as the vertebrae,
is 6 centim. long, exhibits the usual sigmoid flexure, and is
compressed on the external or superior surface as in living Cro-
codiles. Unfortunately the posterior margin of the head is not
quite complete; but from the region of the great trochanter a
powerful muscular ridge, defined by a groove on its anterior side,
runs obliquely downward, outward, and forward, exactly as in the
living Alligator; only the muscular power appears here to have been
greater. The shaft of the bone is similarly subcylindrical ; and the
ridges are distributed in exactly the same way. The inferior surface
of the bone shows the articular head to have been rather better de-
veloped than in the Alligator, apparently a little broader, and cury-
ing a little more inward. The median process is more developed,
and extends as a distinct ridge for a short distance down the shaft.
The muscular tuberosity which represents the lesser trochanter in
Mammals and the trochanter of Dinosaurs generally, seen in the
middle of the shaft, is better developed than in the recent type.
There is an oblique oval depression with an elevated ridge behind
it, and another ridge extending above it proximally. The posterior
ridge runs proximally towards the articular head, and is separated
from the ridge above the muscle by a groove. LHvery thing which
distinguishes the living Crocodile is here intensified.
Proximal end of Right Fibula.
The specimen which Biinzel regarded (pl. vi. figs. 12, 18) as the rib
of a lizard presents all the characters of a small crocodilian fibula,
in which, as compared with living forms, the crocodilian attri-
butes are somewhat intensified. But the bone-tissue is so dense
and brilliant that it has more the aspect of the bone of a bird, Or-
nithosaur, or Lacertilian. The fragment (Pl. XXVIII. figs. 10, 11)
is about 32 centim. long, and has been obliquely fractured below
the expanded head, with a minute displacement which slightly aug-
ments the curvature of the bone. 3
The articular head is relatively thicker than in the Mississippi
Alligator, measuring fully 11 millim. from front to back, and
7 millim. from side to side. The articular surface is somewhat
saddle-shaped as in the living animal, being concave in length and
convex in width. It is widened a little posteriorly, owing to the
development of an oblique muscular ridge, which in the existing
crocodile does not approach so near to the articulation and is less
internal. The internal aspect of the bone is less flattened than in
the Alligator, is similarly marked below the articulation with short
muscular ridges; but they are not defined by a V-shaped area, and
hence the longitudinal tibial ridge, which is well marked proximally,
does not originate in a Y-shaped form. The anterior margin of the
bone is convex from above downwards ; and there is a corresponding
concavity in the length of the posterior outline. The external sur-
FAUNA OF THE GOSAU FORMATION. 687
face was presumably convex from side to side, though (owing, I think,
to crushing) it has a longitudinal groove. There is a small muscular
tuberosity on the outer anterior margin, as in the Alligator, just
where the compressed and curved proximal end merges into the
straight and nearly cylindrical shaft. The shaft at the fracture is
7 millim. long by 6 millim. wide, and has a medullary cavity
which is over 2 millim. in diameter (fig. 11).
UOlna.
With the radius figured by Biinzel, pl. vu. figs. 7, 8, occurs an
ulna. The radius was regarded as that of a lizard. The ulna, which
is slender and compressed, with a somewhat expanded proximal end,
is exactly paralleled by some of the living short-snouted Crocodiles.
The ulna (Pl. XXIX. figs. 9,10) is 63 centim. long, and referable to the
left side of the body; it has the shaft smooth, compressed from side
to side, and contracting and curving aseit descends from the humeral
to the carpal surface. The articular head of the bone (fig. 10) is
remarkably large, being in antero-posterior measurement over 17
millim., while the width is 11 millim. towards the radial border, and
about 1 centim. at the posterior border. This surface is somewhat
concave from front to back. Immediately below the articulation at
the proximal end is a deep impression, which may possibly be due
to pressure, but may also indicate the entrance of a large vessel into
the bone. On the superior aspect there are natural impressions in
the middle of the side and below the inner margin of the articular
surface. The thickness of the shaft just below the articular head is
5 centim.; and though this thickness becomes reduced a little in the
middle of the shaft, there is a slight thickening again towards the
distal end. ‘The width of the shaft just below the articulation is
1 centim.; and this width diminishes to about 6 millim. just above the
distal articulation. On the superior surface of the distal end of the
shaft a ridge appears at the hinder margin, which extends obliquely
across the bone. ‘The distal end is a little crushed and twisted, sub-
reniform, more than | centim. wide, and 6 millim. thick, and makes
an angle of about 45° in the plane of its direction with the proximal
end. The form of the articulation appears to include three regions—
first a deep middle groove, external to which is a small spherical
ball, while internal to it is a concavity. The median groove and the
compression of the bone on the inferior margin give to the articula-
tion somewhat of a broad V-shape.
Radius.
The radius is represented by both right and left bones. The speci-
men figured by Biinzel (pl. vil. figs.7, 3) appears to me to be left. Itisa
straight bone, 6-2 centim. long, corresponding in length with the ulna.
The proximal end (PI.X XIX. fig. 13) of the bone is expanded trans-
versely, with a thickened margin on the inferior border. This end of
the bone is fully 1 centim. wide, but, as preserved, is only: 4 centim.
thick, probably owing to crushing of the superior articular border.
688 PROF. H. G. SEELEY ON THE REPTILE
The shaft (fig. 11) rapidly contracts, so that at a little below the
articulation it is hardly more than 3 centim. wide; but it gradually
expands distally to 1 centim. The bone is compressed from above
downward ; its thickness in the upper half of the shaft is 4 millim.;
but it increases in the lower half of the shaft to over 5 millim.,
owing to the development of a median ridge which divides this part
of the bone nearly equally into internal and external areas, which
are margined laterally by ridges. The inferior surface is also
marked towards the distal end by a slight longitudinal median ridge ;
and the articular end of. the bone 1s subreniform, convex from side
to side. The width of the distal end (fig. 12) is 1 centim.; and its
thickness in the middle is about 3 centim. The distal ridges are an
important distinctive character not found in living Crocodiles.
Cervical Vertebre.
The cervical vertebra are probably about the third and fourth.
What I take to be the third is only the centrum, and, except in less
development of the tubercle for the ribs, differs in no essential point
from the better-preserved bone. ‘The fourth vertebra (Pl. XXX.
figs. 6, 7) might, indeed, be the fifth, sixth, or seventh, since it pre-
sents all the characters seen in the vertebre of the Alligator in the
middle of the neck. It is about the size of the vertebra figured by
myself as that of Crocodilus cantabrigiensis, but is shown to belong
to a distinct species by the less antero-posterior length of the neural
arch, its greater inclination forward, the stronger development of the
hypapophysial spine, and minor characters.
The centrum is 17 millim. long, terminates posteriorly in a well-
rounded articular ball which is about 4 millim. long, and is margined
below by a sharp ridge and above by an equally sharp incised groove
(which may perhaps indicate a certain incompleteness of ossification).
The ball is circular and as nearly as may be a centimetre in diameter.
The cup in front is of corresponding size and form. The hypapo-
physis is a strong compressed process which rises just in front of the
ridge bounding the posterior articulation, and is directed forward
and downward in front of the anterior cup, much as in the fifth
cervical of the Mississippi Alligator. On each side of this process
and below the middle of the side of the centrum, but rather higher
than the corresponding process in the Alligator, is situate the parapo-
physis or articulation for the rib. It blends with the margin of the
anterior cup, and is a strong, compressed, triangular process with a flat-
tened facet which looks obliquely outward and forward. Itis sepa-
rated from the hypapophysis by the usual concave channel (fig.6); and
a similar channel divides it from the diapophysial process on the neural .
arch ; but in the middle of this channel, or, rather, towards its upper
part, is a slight ridge which extends from the upper margin of the
anterior cup backward towards the ball. The diapophysis, as usual,
extends further outward than the parapophysis, and is a smaller
facet supported on a process of which the hinder margin is no more
free than in the third vertebra of the Alligator ; but the process is
FAUNA OF THE GOSAU FORMATION. 689
broad, and defined below and in front by an oblique groove. The
vertical measurement across the two facets for the cervical rib is
1 centim. The neural arch has a decided aspect of being inclined
forward, owing to the way in which the slight rounded ridge from
the diapophysis ascends obliquely forward towards the prezygapo-
physis, coupled with the fact that the posterior border of the neural
canal is straight and parallel to it. The antero-posterior measure-
ment of the eee arch below the zygapophyses is less than a centi-
metre. The sides of the neural arch are concave from above down-
ward, and obliquely channelled. The preezygapophyses are strong pro-
cesses compressed into a wedge-shape in the usual way (fig. 7), directed
upward, forward, and outward, with circular facets, which are divided
from each other by a broad V-shaped notch. The processes are
united by a thin platform above the neural canal, the anterior half
of which is excavated by a longitudinal pit which almost, or quite,
perforates the forked depression between the zygapophyses. From
the hinder half of the neural platform, which has a remarkably four-
cornered appearance owing to the lateral constrictions, rises the
neural spine. It is triangular, being compressed in front and wider
behind, where it is vertically channelled; and the channel descends
‘so as to divide the posterior zygapophyses from each other. The
antero-posterior measurement of the base of the spine is } centim.
Its height, as preserved, from the base of the zygapophysial facet is
1 centim. A slight ridge extends from its anterior border to the
posterior border of the prezygapophysial facet, while in the Alli-
gator the corresponding ridge, when it exists, is carried forward ;
behind this ridge the platform at the base of the neural arch rounds con-
vexly on the side of the centrum. The posterior zygapophyses (fig. 6)
are strong wedge-like processes directed outward, only slightly ex-
tending behind the neural spine, and not entirely behind it as in the
Alligator. They are remarkable for the well-defined notch below
them, something like that seen in the third and fourth vertebre of
the Alligator, and for the tubercle above the posterior margin of the
ovate facets, which gives the back of the zygapophyses a sce
channelled appearance, to which the Alligator offers no parallel.
The measurement from back to front over the zygapophyses is
2centim. The transverse measurement over the preezygapophyses
is about 18 millim. The side-to-side measurement of the constric-
tion between the anterior and posterior zygapophyses is 12 millim.
The posterior zygapophyses were evidently narrower than those in
front by a millimetre or two. The neural canal is transversely ovate
behind, but in front appears wider and more depressed (fig. 7), with
a flat sail: the floor of the centrum is concave, and shows the usual
pair of nutritive foramina.
Dorsal Vertebre.
There are 8 dorsal vertebre, which mostly belong to.the hinder
part of the series. Reckoning as the first dorsal that vertebra in
which the rib is for the first time entirely carried on the transverse
process, I should regard the earliest vertebra preserved of this
Q.J.G.8. No. 148. 22
690 PROF, H. G. SEELEY ON THE REPTILE
series as probably not later than the 6th dorsal, while it might have
been as early as the second, which is likely to have been its true
position. Then succeeds a centrum which may have belonged to
about the fifth dorsal. The remaining six vertebree appear to be in
sequence, and belong to the hinder part of the vertebral column;
and if the number of vertebre was the same in this animal as in the
Alligator, they might be the 7th to 12th dorsal vertebrae. The
13th, or last dorsal or lumbar vertebra, if found separately, might
have been referred to another genus, and perhaps to a Dinosaur.
The first sacral vertebra is impertfectiy preserved.
The early dorsal vertebra is distinguished, as in existing Croco-
diles, by the sight development of the ridge, which ascends from the
hinder border of the preezygapophysis inward and backward towards
the neural spine. The centrum has a length of from 18 to 19 millim.;
so that there is but little increase of length as compared with the
cervical region. The transverse process is compressed and directed
outward horizontally or a trifle upward. It is thickened on the in-
ferior posterior border by a ridge which extends downward towards
the centrum and constitutes a marked specific character, especially
as there is a deep conical pit behind it immediately below the notch
which separates the transverse process from the postzygapophysis.
The antero-posterior width of the transverse process is 11 millim.
Resting upon it in front, rather more horizontally than in existing
Crocodiles, so far as regards its lateral direction, is the preezygapo-
physial facet (fig. 8), which i is about 11 millim. long and 6 millim. wide.
The transverse process is perhaps a little lower in position than the
transverse process in the early dorsal vertebre of the Alligator, being
on a level with the upper part of the neural canal. The ridges on
the posterior zygapophyses are rather narrow, so as to give a some-
what pinched aspect to the concave area on each side at the base of
the neural spine (fig. 8). The neural spine extended backward a
little between the diverging ridges of the posterior zygapophyses ; and
at its base there is a pit. The centrum is evenly rounded (fig. 9),
and both cup and ball well developed. As in the cervical region,
the ball is marked on its upper margin by an incised groove (fig. 8)
similar to that seen in the vertebra of the Alligator.
The later dorsal vertebrae, as in existing Crocodiles, are charac-
terized by the deeper depression between the anterior and posterior
zygapophyses, and by the increased elevation of the zyg apophyses
above the transverse process, consequent upon this process acquiring
a somewhat lower position relatively to the neural canal. The pre-
zygapophyses come to extend a little further forward and to look a
little more upward and inward. The centrums increase in length
so that what I regard as the tenthis 23 millim. long. The articular
cup in front, perhaps, becomes a little wider; and “the base of the
centrum is rather more flattened. ‘The compressed appearance at
the base of the transverse process gives place to a regular concavity
from above downward ; and the antero-posterior extent of the neural
arch is increased, while the size of the neural canal is diminished
and its height lessened. There also comes to be a less development
FAUNA OF THE GOSAU FORMATION. 691
of the inferior margin of the cup of the centrum, which gives a slight
appearance of leaning forward to the bodies of the vertebre. The
twelfth centrum is 22 miilim. long, and has the cup 13 millim. wide
in front, showing an increase in the depression of the centrum simi-
lar to that which is observed in the later dorsal vertebree of existing
Crocodiles.
Lumbar Vertebra.
The lumbar vertebra (Pl. XXX. figs. 10, 11) may not have been
the only one of its kind; it certainly did not immediately succeed
the last dorsal, if it is supposed to have pertained to the sams
animal; for it has the centrum much more depressed, with the zyga-
pophysial facets perceptibly higher, but still retaining a much less
inclined position than is seen in the Alligator. The cup in front of
the centrum (fig. 10) is 1} centim. wide, and, as preserved, 1 centim.in
vertical diameter ; so that it has a transversely oval form, which gives
a broad aspect to the base of the centrum. The posterior ball has a
similar pterodactyle-like transverse extension, but, as in the earlier
vertebree of the series, is margined above by the characteristic groove.
The transverse process is only 7 millim. wide at the base, and was
therefore small, hke the corresponding process in the Alligator.
In transverse section (fig. 11) it is somewhat T-shaped, owing to the
development of an inferior sharp vertical ridge which descends to
the base of the neural arch, widening as it comes downward. This
ridge curiously resembles that which is so characteristic in the neural
arch of a Dinosaur; but it is clearly comparable to that which I have
referred to in the early dorsal vertebra, and constitutes one of the
distinctive characters of the species. The neural canal here enlarges
again as though in anticipation of the sacral expansion. The notch
between the posterior zygapophyses is wider in this vertebra than in
the dorsal series; and the zygapophyses appear to be somewhat
stronger and broader.
Sacral Vertebra.
The first sacral vertebra is only a fragment, the greater part of the
neural arch being broken away, only a portion of it remaining at the
anterior end of the left side. The centrum is remarkably oblique; it
is 2 centim. long, and flattened on the under side, with a small median
grooye in the anterior part. ‘The sides are rounded; the anterior cup
is imperfectly preserved, but appears to have been more depressed
than in the lumbar vertebra. The posterior end of the centrum is
oblique, flattened, with a depression below the neuralsurface. It is
narrower than the anterior end, being about 11 millim. wide, as pre-
served, and semicircular in outline. The basal surface of the neural
canal is smooth, straight, and concave from side toside. The neural
arch enters into the anterior cup as in the Alligator, and gives oif at
the anterior end of the side a massive transverse process, the frac-
tured base of which is 13 millim. deep and 1 centim. wide, and has
a somewhat reniform outline owing to the anterior concavity. Only
the base of the anterior zygapophysis is preserved.
222
692 PROF. H. G. SEELEY ON THE REPTILE
Caudal Vertebre.
The early caudal vertebra was probably about the fifth or sixth.
The late caudal vertebra would correspond with about the 23rd or
24th in the Alligator, though the form of the centrum might be
taken to indicate that the tail was relatively short, and probably
contained fewer vertebrae, while, from the absence of any continued
series, its identification as belonging to this species is open to some
doubt. The early caudal vertebra (Pl. XXX. figs. 12-14) is of
elongated form, compressed at the sides, narrow and somewhat flat-
tened on the underside. The length of the centrum is 31 millim.
The cup in front (fig. 14) is circular and 11 millim. in diameter;
below it is an oblique hypapophysial facet. The cup is slightly
oblique ; and the length of the base of the centrum is 22 millim. Pos-
teriorly the outline is subquadrate, owing to the flatness of the sides
and to the development of two facets divided by a groove below the
articular ball (fig. 13). Unlike the Alligator, the centrum is widest
over these facets. There is the incised margin on the upper surface
of the ball which characterizes all the vertebree. The width of the
posterior end of the centrum is | centim., its extreme depth 13 millim.
The centrum has a pinched-in appearance (fig. 13) below the trans-
verse process (fig. 12), which, as usual, was given off about the middle
of the side, was horizontal, compressed from above downward, and,
though convex on the underside, shows no indication of a ridge.
The antero-posterior extent of its base is about 12 millim. The
neural arch appears to have had avery short neural spine; and the
ridges from the zygapophyses, instead of being directed downward to
join the transverse process as in the Alligator, converge inward and
backward to form the base of the neural spine in front. The ante-
rior zygapophyses projected in front of the centrum ; the facets (fig. 12)
looked more upward and less inward than in the Alligator ; and there
was no notch between them exposing part of the neural surface of
the centrum.
The late caudal vertebra, supposing it to belong to this species,
concerning which I feel some doubt, is about 17 millim. long, has a
ridge in place of the transverse process, has the narrow base mar-
gined by two sharp parallel ridges, and the posterior cup deeper
than the anterior cup.
Teeth.
There are 5 Crocodilian teeth. The most important of these
(Pl. XXVII. fig. 25) is fractured, but appears to indicate an ovate
crown curved slightly inward, terminating on each side in a strong
ridge, and having the exterior face marked with a number of faintly
elevated blunt strie, with finer striz on the inner face; the crown,
which is a little worn, is 1 centim. high, and gives indication of the
beginning of the fang. There are two successional teeth; one of
these has a circular base, the other an oval base; both are short and
blunt, marked with lateral ridges and covered with numerous fine
parallel striz. The largest is nearly 4 centim. in diameter (fig. 24).
FAUNA OF THE GOSAU FORMATION. 693
Another tooth has the same general character; but the crown
appears more curved, with sharper lateral ridges and finer and more
numerous striations.
In the possession of lateral ridges, as well as in the striated sur-
face of the crown, the teeth of this species approximate to those re-
ferred by Leidy to Hyposaurus; but there is no correspondence in
vertebral characters. ‘he vertebre referred by the same author to
Thoracosaurus correspond in being proceelous, but differ in the posi-
tion and character of the tubercles for the articulation of the ribs, as
well as in the form and direction of the neural spine in the cervical
region. Itis difficult to determine accurately the relation of the
species to Holops ; but the absence of the hypapophysis from the early
dorsal vertebre will exclude comparison with that form, equally with
the contour of the neural canal. Holops, however, appears to have
had the sharp ridge margining the parietal bone which is seen in
the specimen figured by Biinzel.
It is impossible to determine whether the parietal bone of Croco-
dilian character (figured by Bunzel, pl. 1. figs. 1-2), is referable to
this species or to some other animal. Its distinctive features are the
sharp lateral ridges margining the temporal fosse, the fineness of
the circular pits on the bone, and the remarkable thinness of the
bony substance.
That this species can remain in the genus Crocodilus is impro-
bable; but at present I see no grounds on which to separate it.
PLEUROPELTUS SuEssII, Seeley.
Postfrontal Bones of a Chelonian Skull.
Two fragmentary bones (Pl. XXVIII. figs. 8, 9), right and left,
present on their external surface impressions of scutes, and on their
under surface portions of a large cavity which I believe to be orbital ;
therefore I interpret these fragments as being postfrontal bones of a
large Chelonian of Emydian affinities; and as the skull, when com-
plete, was obviously of large size, it may well have belonged
to the animal indicated by the large costal plates presently to
be described. The remarkable feature about this bone is the
character of its sutures; for while a groove runs round the thin
margin in which the edge of the bone terminates, and evidently
received a sharp ridge from the adjacent bone, the margin on the
under side is bevelled, and thus demonstrates a union of the bones
by squamous overlap. The under surface of the bone (fig.9) is crossed
by an oblique ridge, which divides it, as preserved, into two nearly
equal portions. This ridge helps to form a part of the posterior
boundary for the eye-ball, and is characteristic of Chelydra and
allied genera. ‘The orbital surface is concave, and more resembles
that of Chelydra serpentina than that of T'rachydoglossus; and the
resemblance extends even to the position of the vascular foramen
at the back of the orbit, though there may, perhaps, in the fossil be
several small foramina in aline. This surface, as preserved, mea-
694 PROF. H. G. SEELEY ON THE REPTILE
sures about 4 centim. in its greatest length, and upwards of
3 centim. in its greatest width. The bone probably extended for-
ward no further than the middle of the orbit; and in that case but a
small portion is lost. The area posterior to this ridge bounding the
back of the orbit is excavated, 4 centim. long and 2 centim. wide.
It consists of an inner oblong area, truncated externally by the
suture for the malar bone, and margined by the bevelled edge re-
ferred to, which is about 6 millim. wide behind and 8 millim. on the
inner side. The superior surface of this subquadrate fragment (fig. 8)
is convex from within outward, showing that the top of the head
was flattened, but that it rounded into the lateral area. It is divided
into seven areas by unusually wide and well-marked scutal grooves.
The bone between these grooves has a roughened, somewhat pitted
appearance, indicative of vascular structure. The scutes are espe-
cially remarkable from their number and small size; that over the
orbit is largest, being about 3 centim. long and more than 14 centim.
wide. The other scutes will be best understood from the figure.
They are irregular, subquadrate or subtriangular figures, varying in
measurement from 1 centim. to about 14 centim. The grooves which
define the scutes are from 2 to 3 milliim. wide. The articular sur-
face for the malar bone (fig. 9) 1s 27 centim. long, and over a centi-
metre deep. It is a concave shallow groove, which involves the ter-
mination of the postorbital ridge. There is every reason to suppose
that the squamosal articulation was a small area just behind the
malar articulation, and that it did not extend for more than a centi-
metre. Hence the inner and posterior bevelled articular surface,
which becomes very thin behind, is related to union with the parietal
bone. The posterior portion is oblique, and makes an angle of 45°
with the interior portion, which is straight and parallel to the
orbital margin. Three scutes are crossed by the parietal suture,
which, indeed, is the case in the skull of the Common Turtle. In
front of the parietal suture, commencing with the most anterior
inner scute, is a distinct suture, which prolongs the line of the
parietal, and therefore gave attachment to the frontal. The portion
of the right postfrontal bone includes four scutes and a fragment
of the inner part of the postorbital ridge, extending as far forward
as the termination of the parietal suture.
Oostal Plates.
Dr. Biinzel figured a remarkable specimen, which he regarded as
the left ilium of an animal named Danubiosaurus anceps, the sup-
posed rib of which proved to be a Dinosaurian scapula. I find a
second specimen of this supposed ilium, less perfect, but similar in
character, evidently coming from the opposite side of the body. For
reasons to be mentioned, I have no hesitation in interpreting these
specimens as ribs to which dermal plates are ankylosed. But there
is something very different here from what is observed in ordinary
Chelonians ; and though I have no doubt that we have to do with
a pair of Chelonian costal plates, the type indicated by these re-
mainsisnew. It would, indeed, have been less startling to refer the
specimens to any part of the skeleton of a Dinosaur or lizard than
FAUNA OF THE GOSAU -FORMATION. 695
to the Chelonia; for these fossils, if rightly interpreted, indicate an
animal with a relatively larger vertebral column than any Chelonians
now known, or at least with a vertebral column constructed upon a
different plan. The ribs were wide, as in the marine Chelonia, and
extended distally far beyond the limits of the plates which covered
them. The superimposed plate is developed chiefly behind the rib ;
its anterior margin is smooth and rounded; the posterior margin is
not preserved, but obviously became thin. ‘The free articular end
of the rib was massive ; and the superimposed plate extended beyond
it proximally for an unusual distance, indicating great width for the
intervening vertebra. ‘his portion of the dermal plate, which extends
mesially beyond the rib, has the external surface well preserved, but
wants the smooth ossified internal surface; and as this is absent in
both specimens, it is possible that m the living animal this internal
part of the plate may have been cartilaginous or united to other
bones. Neither of the specimens gives the slightest indication either
of external scutes or ornament, or of union to adjacent bones; and
the external surface is such as would suggest that the bones were
probably contained, if not beneath a muscular covering, at least
beneath a skin which had not become specialized ; so that we have
here an animal that in some respects recalls the Protostega of Prof.
Cope, but differs essentially in the dermal plates being blended
with the ribs. An allied but undescribed type from the Cambridge
Greensand also has the costal plates separate from each other, but
differs in having them marked with scutes.
A short description of each of these specimens appears neces-
sary. First, the less perfect of the two (Pl. XXX. fig. 15)
shows a smooth external surface gently convex in length and
somewhat convex from side to side. It consists of a thick dense
dermal plate superimposed upon a rib, this plate probably being
a representative of the supracostal cartilages and ossifications
found in birds, crocodiles, and Hatterra. Immediately above the
articular expansion of the rib, at the proximal end, the plate is a
centimetre thick, and is defined by the density of its texture from
the osseous matter of the rib beneath. This bone on the interior
suriace is much eroded, but presumably extended much further to-
wards the median line of the animal’s body, since the dermal plate
is prolonged with a rough under surface, due to this bone having
adhered to the bone with which it is blended; and as the plate is
prolonged mesially, its thickness becomes reduced to one half, though
the fractured specimen is imperfect at its margin. ‘The transverse
width of the plate, as preserved above the expanded head of the rib,
is about 94 centim. About 9 centim. further away from the
middle line of the animal, a length of about 4 or 5 centim. of the
margin of the plate is rounded; and here its union with the thin
underlapping, transversely expanded margin of the rib is distinctly
seen. On the opposite or posterior margin there are some faint
indications of a lateral rounding of the margin of the dermal plate.
At 18 centim. from the proximal end of the rib the dermal plate
comes to an end, being broken away, and.allows the rib to project
freely from under it, showing, I think, that although there was
696 PROF. H. G. SEELEY ON THE REPTILE
bony union between these two parts of the skeleton, it was a union
established somewhat late in the animal’s life. At this point the
bony plate is somewhat thinner than at its proximal fracture; the
plate tapers apparently outwards, and is somewhat broken away
from the anterior proximal margin of the rib. The plate is hence,
as preserved, of a lanceolate form; but its outline cannot be accu-
rately stated.
The rib in this specimen differs from the ribs attached to the
costal plates of living Chelonians in being coextensive with the plate
—that is, as wide as the plate, and, as shown by the other specimen,
as long; hence its limits are not defined distinctly in any part of
its extent, least so in the proximal part of the bone, where the sur-
face is convex from side to side. This convexity becomes narrower
and relatively more elevated as the bone proceeds outward, and is
confined to its anterior border; where the rib terminates it is over
3 centim. wide, over 1 centim. thick, and, though compressed on
the anterior border, is more compressed on the posterior border.
The thickness of the combined rib and plate is about 24 centim. ;
but even as preserved, the thickness at the fractured articular end is
7 centim. The underpart of the bone, which is slightly displaced by
a fracture consequent upon a minute dislocation, is convexly rounded
from side to side, and concave from within outwards, so as to pre-
sent a saddle-shape. ‘The transverse width of the fragment pre-
served is about 64 centim. The anterior border is notched, as
though for the passage of an intervertebral nerve, or from the head
of the rib being free, as in ordinary Chelonia, though the conforma-
tion would rather suggest the former interpretation. There is one
curious character in evidence that the expanded lateral part of the
rib extended further towards the middle line than the articular
head, showing that the ribs had attained an unusual transverse de-
velopment consequent upon the expansion ot the superimposed
plates. The transverse width of the head of the rib is 4 centim. ;
and here the fracture gives it an almost semicircular outline.
The second specimen, already figured by Bunzel, pl. vi. figs. 4,5, has
a length, as preserved, of 48 centim.; of this 39 centim. is occupied
by the blended rib and its superimposed dermal plate, the remaining
9 centim. consists of the extension of the plate alone beyond the head
of the rib towards the middle line of the body. The plate, where it is
presumed to have extended over the vertebra, is thin, and becomes
thinner the further it extends, both mesially and laterally. Its mar-
gins are imperfectly preserved, but have a wedge-shape. The costal
region wants a small portion in the middle of the plate in front ;
but throughout it has the anterior margin preserved rounded from
below upwards, and roughened in the proximal half, as though with
ligamentous attachment to the adjacent plate. On the upper surface
these lines at first run in a transverse direction, and then run for-
wards and inwards, just as on the under side they run downward
and outward. This oblique direction is strongly suggestive of the
oblique crossing of ordinary intercostal muscles. In length the
anterior margin of the bone is gently concave. The posterior margin
FAUNA OF THE GOSAU FORMATION. 697
is, unfortunately, not preserved; and the plate is remarkably con-
vex from before backwards above, though this convexity is more
marked on what I take to be the posterior side than on the anterior
side. The extreme width of the plate below the articular head of
the rib is about 133 centim.; and it gradually tapers as it extends
outwards. JDistally the thickness of plate and rib diminish; and at
the extreme distal end, where the transverse measurement, as pre-
served, is under 3 centim., the thickness of the combined plate and
rib is less than a centimetre. The posterior half of the plate, while
smoother externally than the anterior half, is marked with several
short, parallel, straight, vascular grooves, which are very narrow ;
each is about 2 centim. long. This condition leads me to suspect
that the anterior part of the rib may have been imbedded in muscle,
while, owing to its curvature, the middle of the plate may have had
only a dermal covering.
The interior or under side of the specimen has the expanded head
of the rib broken away ; and while it was placed in the middle of
the width of the plate as in the other specimen, the rib soon be-
comes developed on the anterior border, being limited by a concavity
which runs down the length of the bone, dying away with the ele-
vation of the rib at the distal end. This principal part of the rib
becomes narrower as it extends further outward; but the fractured
condition of the posterior margin appears to indicate that the margin
of the rib was prolonged as a thin film towards the adjacent plate.
No similar remains which are referable to an animal of this kind
have been discovered.
Scapula of large Chelonan.
The fragment which | identify as a portion of a right Chelonian
scapula, indicates an animal of somewhat large size. It shows no
trace either of the preecoracoid or the articular end of the bone, which
had decomposed prior to fossilization, or of the distal end ; so that it
is not a fragment giving valuable information concerning the affini-
ties of the animal. The fragment 1s 9 centim. long, 4 centim.
wide at the proximal end, as preserved, and 2 centim. wide at the
distal end. The surface which { take to be posterior is smooth,
convex from side to side, but more flattened at the distal end than
at the wider proximal end. In length the surface is almost straight.
The internal margin is concave and sharp, and looks as though it
might have been produced into a preecoracoid. The external margin
is shghtly convex, except towards the proximal end, where it is
modified, owing to the bone bending outwards and downwards, as
though for the formation of the articular surface. The anterior
aspect of the bone is much rougher; and there is a ridge which
becomes stronger towards the proximal end, thickening the bone
on its outer part, and making it concave in length, and dividing the
anterior aspect into a broad, flattened, inner area and a narrower
external area. The thickness of the bone towards the proximal end,
where fractured, is 2 centim., and the thickness towards the distal
698 PROF, H, G. SEELEY ON THE REPTILE
fracture 13 millim. This is not an identification in which I feel
absolute confidence, on account of the smoothness of one side of the
bone and the roughness of the other, which [ had not noticed in any
Chelonian scapula.
Emys Neumayert, Seeley.
There occur many remains of several Chelonians of moderate size.
I only brought to this country a selection of some of the more cha-
racteristic fragments, which all belong to the carapace and plastron.
It does not seem to me desirable to determine the genera from these
specimens ; but from their general character rather than from any
distinctive characteristics, | regard them as being Emydian. The
specimens are as imperfect as any of the other reptile remains, and,
as they do not differ much in size or character, are difficult to deal
with. ‘There are, however, certain differences of texture and form
which justify me in indicating the existence of several species.
These are all referred provisionally to the genus Hmys, pending
better evidence of their generic characters. ‘The species are best
distinguished by the characters of the plastron; for the hyo- and hypo-
plastral bones preserved may indicate, even in their fragmentary
condition, four species. The bulk of the remains I refer to the
largest species, which was fully 25 centim. across the carapace.
This species is marked by the depth of the grooves which define the
areas of the scutes, and frequently by their elevated borders. Another
marked feature is the exceedingly fine subgranular condition of the
bone on its external surface—a character difficult to define, but
altogether peculiar. Of this species the plastron is represented by
portions of the hyoplastral and hypoplastral bones, though from their
fragmentary condition, it is not always easy to distinguish between
these. One fragment (Pl. XXX. fig. 16) is only 73 centim. broad and
54 centim. long ; it does not show a single sutural surface, but exhibits
the axillary region crossed in its lower part by an oblique scutal im-
pression which runs forwards and a little inwards till it reaches the
inner margin of the preeaxillary scute, which is prolonged forwards
on the superior edge as a strongly marked groove. The usual trans-
verse scutal impression on the basal part of the hyoplastral plate
runs a little in advance of the axilla, and, as it nears the lateral
margin, is directed angularly forwards in the last centimetre of its
length. This scutal impression is strongly elevated; the ascending
axillary process was compressed and directed obliquely upwards,
forwards, and apparently a little outwards. The thickness of the
plate varies from 3 centim. in the inner part to 1 centim in front of
the axillary notch.
A second specimen, showing the anterior part of a similar right
hyoplastral plate, may, perhaps, belong to the same species though
to another individual: the thickness of the scute is the same; the
elevated ridge at the scutal suture is the same; though fractured in
front, it measures upwards of 44 centim. anterior to the trans-
verse suture. The lateral margin of the plate is sharp, being be-
FAUNA OF THE GOSAU FORMATION. 699
velled above, with the bevelled area also defined internally by a
sharp ridge, interior to which runs a slightly impressed broad prolon-
gation of the supraaxillary impression. In the carapace no neural
plate is preserved. The first costal plate (Pl. XX XI. fig. 13) on the left
side is nearly perfect; it is slightly arched, rather less than 10 centim.
long, and more than 33 centim. wide at the lateral impression of the
first vertebral scute. It shows the oblique sutural surface for the
nuchal plate, which has a concave border about 35 centim. long ; the
width of the union with the first neural plate is 22 centim., but was
probably more, as the posterior border of the moat 1s imperfect.
The rib is not visibly distinct from the plate upon which it is sup-
ported, as it is in some species of V’estudo; it has a well-elevated
compressed head, 7 millim. deep and 4 millim. wide; it is placed
obliquely, so as to look forward and outward. In the middle of
the plate the rib has become so depressed as to be only just recog-
nizable; it is there 1 centim. wide; but at the outer part of the
plate its extremity is prolonged beyond the plate, to unite appa-
rently with the marginal plate. Anterior to it, on the under
side, the plate is excavated (Pl. XXVII. fig. 27), and the side
of the rib roughly striated, owing to attachment of the supra-
axillary process from the hyoplastron. This excavation extends
inwards from the extremity of the rib for 44 centim. A fragment
of the right plate shows its depth where it joins the first neural
plate to be 34 centim., and the greatest depth of the bone to be
about 4 centim. ‘There are several fragments of costal plates ; but
they can only be identified by the scutal markings. What appears
to be a third costal plate of the left side is impressed with the trans-
verse border dividing the second and third vertebral scutes for a
length of 32 centim.; and since at this point the antero-posterior
measurement of the plate is only 3 centim., it shows that the ver-
tebral scutes were extremely broad relatively to their length, since
the length could not have exceeded 6 centim., while the breadth
could hardly have been less than 10 centim. The plate is arched,
showing that the carapace was as much elevated as in a testudinate
Chelonian. Its extreme length, without reckoning the curve, is
upwards of 11 centim.; following the curve, the length is nearly
13 centim. The breadth of the plate, towards the outer margin,
is about 34 centim. Its thickness at the proximal part is 4 millim.,
and at the distal end 3 millim. On the under side the head of the
rib is moderately elevated; but its course down the plate is only just
perceptible, and marked by a smoother condition. It does not ap-
pear to have been prolonged at the distal margin. A plate from
the hinder part of the carapace, which is imperfect, also shows the
arched character strikingly. It is remarkable for its antero-posterior
extent of nearly 33 centim., and appears to be the last costal plate.
If so, it is impressed on its outer part with a vertebral scute. Hence
T infer this animal to have had a nearly circular outline, and to
have had the shield greatly elevated. It may be distinguished as
Emys Newumayrt.
700 PROF. H. G. SEELEY ON THE REPTILE
OTHER SpEcIEs oF Emmys.
Another species, represented by the remains of more than one
example, is, however, known chiefly from the hypoplastral plates.
It appears to have been a smaller species than the last, though it is
not easy to estimate its size from the distance between the axilla,
or from the breadth of the abdominal scutes. The hypoplas-
tron shows some indication of the median and anterior sutural
margins, which would indicate a broad species, after the pattern of
the foregoing. The length of the fragment is 64 centim., and its
breadth about 6 centim. The transverse scutal impression is from
24 to 3 centim. behind the anterior suture. The bone is compressed
to a sharp margin, which is prolonged as an elevated ridge for about
1 centim. beyond the inguinal notch. The margin is nearly straight.
I regard this ridge as indicative of a well-marked species.
A third species is distinguished by the way in which the axillary
and inguinal processes are obliquely overlapped. A fourth species,
of small size, is represented by many parts of the carapace and
plastron.
ARMOSAURUS GRACILIS, Seeley.
Vertebra.
The vertebra of a lizard, figured by Bunzel, pl. vi. fig. 11, 1s very
imperfect, and so badly drawn as to give no just idea of its cha-
racters. It is remarkable for the perfectly globular form of the
posterior articular ball, which is nearly 6 millim. in transverse
measurement, and nearly 5 in vertical measurement. It is margined
by an impressed groove, which extends further forward on the
neural margin than on the visceral margin. The length of the cen-
trum in the middle line is 13 millim. What remains of the an-
terior cup is deeply excavated to correspond with the articular
ball, with a sharp margin conspicuous on the inferior border. The
inferior interarticular surface of the centrum is 1 centim. long; on
its base run two parallel blunt ridges, divided by a median groove ;
external to these ridges are two oblique impressed concave lateral
areas, which are broad in front and narrow behind, margined
superiorly by an oblique rounded ridge, which ascends from the
upper margin of the articular ball towards the middle of the arti-
culation for the rib on the anterior part of the vertebra. This arti-
culation for the rib is a strong process, extending laterally further
than the width of the articular cup of the centrum, is concave from
above downwards in front, looking obliquely downward and out-
ward, long and narrow, rounded from fore to back, and most
elevated proximally. It carries superiorly the prezygapophysis,
which was a large oval surface, looking upwards and a little inwards,
placed just above the articulation for the rib, and considerably above
the intervertebral articulation. The zygapophysis is only preserved
on the left side, the portion which had existed on the right side
FAUNA OF THE GOSAU FORMATION. 701
haying disappeared before the bone came into my possession. It is
impossible from this slender evidence to determine the affinities of
this animal.
OrnitHocHErRus Bunzett, Seeley.
The remains of Ornithosaurians are unsatisfactory, being, for the
most part, either small portions of shafts of bones, or else bones
which have been greatly crushed. ‘The fragments of phalangeal
bones throw no light on the structure of the animals to which they
belong, and give no clue to specific characters. The bone-tissue, how-
ever, is somewhat thicker than in English specimens ; and I have no
doubt the fragments belong to a peculiar species. There is an in-
teresting crushed proximal end of a humerus, showing the form of
the head, the immense radial crest, and the ulnar expansion of the
bone at the humeral articulation: and this, with some other frag-
ments, characterized by thin texture of the bone, may, perhaps,
indicate a second species. But although of great local interest as
demonstrating the presence of these animals in a period of time
in which they were so plentiful in England, these fragments are
of no importance to the anatomist. The only specimen of import-
ance is the articular end of the lower jaw, already described by
Biinzel (pl. vi. figs. 6,7). This bone is obliquely fractured just
in front of the articular end, and shows the articular surface
and the characteristic keel beyond it. The length of the fragment
is 34 millim. The bone is compressed from side to side; and the
sides converge downward into a narrow rounded ridge. The ex-
ternal surface is flattened like the internal suriace, which latter
shows a suture with very irregular margin, nearly parallel to the
base, and near to it, indicating that the articular bone was re-
ceived into the angular bone. The area in front of the articula-
tion contracts from side to side, and is rounded; but on the inner
margin there is a large pit partly fractured through, indicating a
pneumatic foramen. ‘The articular surface is transversely ovate in
area, with a median ridge running obliquely backwards and outwards
from the hind margin of this foramen. This divides the articular
surface into a triangular concave area in front and towards the
outer side, and a posterior groove which is best developed towards
the inner side of the jaw. ‘This articulation perceptibly widens the
bone at each side. Its width is 13 millim., its length 8 millim.
Behind the articulation there is no defining border, like the sharp
elevated ridge in front, but the surface is flattened, with the sides
slightly converging till they terminate in the rounded extremity.
This posterior area is directed obliquely downwards to the base of
the bone. The inner half of its surface consists of a pneumatic
foramen, which is 13 millim. long, and reaches forwards to the
posterior articular groove. This jaw seems to be well distinguished
from the species already described.
702 PROF. H. G. SEELEY ON THE REPTILE
CoNncLUSION.
From this survey it appears that Dinosaurs were well represented
in the Gosau beds. Most of the remains belong to two species of a
quadrupedal carnivorous genus Cratwomus, which in many respects
resembles Scelidosaurus. It is just possible that Struthiosaurus
may prove to be the same genus, or may have possessed the teeth
referred to Cratwomus. The genera Hoplosaurus, Oligosaurus, Rha-
dinosaurus, and Ornithomerus are only known from a few bones
each ; Meyalosawrus merely from teeth. It is just within the limits
of possibility that Doratodon may prove to be the jaw of Rhadino-
saurus; but it is not likely to belong to the Crocodile, because true
Crocodilian teeth occur. Hence there are certainly, with the Moch-
lodon, seven Dinosaurian genera, while there may be as many as ten
genera. Of Crocodiles, Lizards, and Pterodactyles there are certainly
at least one each. The Chelonians are represented by two genera
and five species, two only of which are described. Thus the Gosau
fauna includes in all fourteen genera and eighteen species of reptiles ;
and there is every reason to suppose that these formed but a part of
the Reptilia living when the deposits were formed.
I can scarcely hope that my efforts have been in every case suc-
cessful in determining the species to which these disjointed and
often fragmentary bones should be referred; but I have throughout
worked on the basis of anatomical structure, and indicated only
such species and genera as the organization of the animals made
inevitable.
I have now only to express my gratitude to Professor Suess for
his kindness in allowing me to study this collection and retain the
specimens so long in this country; and I would also express my
thanks to Prof. Ramsay for permission to figure the skull of Acan-
thopholis ; and to the Council of the Royal Society for assistance in
carrying on this research.
APPENDIX.
Norte on the Gosav Buns of the Nrvz Wert, Wusr of WIENER
Nevsrapt. By Prof. Epwarp Suzss, F.M.G.S.
Tue Gosau beds have been deposited in preexisting valleys of the
Triassic and Rheetic portion of our North-eastern Alps, and have
suffered so much subsequent folding and dislocation that in the
valley of the ‘‘ Neue Welt,” the spot where the bones were gathered
which I sent to you, several shafts pass twice through one and the
same seam of coal. The Gosau beds usually form green slopes at
the foot of the great mural precipices of Triassic and Rheetic limestone.
In the Gosau valley, near Halstatt, exposures are offered by a series
FAUNA OF THE GOSAU FORMATION. : 703
of ravines; in the ** Neue Welt ” (south of Vienna, west of Wiener
Neustadt) a number of coal-mines give the opportunity of following
the succession of beds, although they are highly disturbed here; and
I believe that the succession is not very different in the two valleys,
notwithstanding their distance apart.
The base of the Gosau beds is formed by a calcareous breccia of
variable thickness, evidently the consolidated débris of the surround-
ing mountains.
Then follows a series of freshwater beds, sandstones, marls and a —
few seams of coal, accompanied by freshwater Mollusca such as Mela-
nopsis, Dejanira, Boysia, Tanalia, Cyclas, and Unio, and the remains
of a highly heterogeneous flora, comprising a true Palm, together
with Pecopteris Zippi, Microzama, Cunninghanuites, and leaves of a
dicotyledonous tree resembling Magnolia, &c., evidently the ming-
ling of the younger dicotyledonous type with a number of survi-
ving older types. It is this horizon which has yielded the reptilian
bones.
Deposits of a brackish character, with Cerithiwm, Omphalia, and
Acteonella, begin to appear above the freshwater beds, sometimes
apparently intercalated with them and accompanied by gravel
beds and conglomerate, sometimes also by the first true marine
strata, usually characterized by Hippurites organisans and Nerinwa
breincta.
The next group is formed by a loose marly limestone ora cal-
careous marl crammed with reef-building corals and with masses of
Hippurites cornu-vaccnum, Hipp. sulcatus, Caprina Aguillona,
Spherultes organisans, and a good number of highly ornamented
Gasteropoda. This is the true French Turonian zone of Hippurites
cornu-vaccinum.
This zone is succeeded by a series of loose grey and marly sand-
stones, likewise very fossiliferous. ‘The reef-building corals and
Rudistez have disappeared or are very rare, corals being represented
by a few species of Cyclolites, by Diplochenium lunatum and especially
by Troechosmilia complanata. Here the first Ammonites appear.
Natica bulbiformis, Cardium productum, Protocardia Hillana,
Trigoma limbata, and Janira quadricostata are some of the most
characteristic fossils.
In some places rose-coloured limestone beds with Orbitoides and
the remains of a small Decapod are seen, which seem to succeed
directly to this zone, which I have sometimes named the zone of
Trochosmilia complanata.
The last and highest member of the Gosau beds is a series of
sandy loose sandstone beds, containing no fossil except great
numbers of Jnoceramus Crispi.
I cannot, therefore, say positively that the age of the reptiles
which you have had the kindness to study is quite exactly that of
your Cambridge phosphate-beds ; but it is certain that they are older
than the true Turonian deposits, and especially older than the zone
of Hippurites cornu-vaccinum.
704
PROF. H. G. SEELEY ON THE REPTILE
EXPLANATION OF PLATES XXVII.-XXXI.
(All the figures are of the natural size, unless an enlargement is mentioned.)
Or
Puare XXVII.
. Dentary bone of right ramus of lower jaw of Mochlodon Suessii (Bunzel)
seen from above, showing tooth-sockets, symphysial curvature, and
ascending coronoid process.
. Separate tooth of Mochlodon Suessii from the lower jaw, showing the
internal aspect; enlarged twice.
. Tooth referred to the upper jaw of Mochlodon Suessiz, showing the
ribbed external face of the crown; enlarged twice.
. Side view of the same tooth, showing the worn internal edge of the
crown and curved fang.
. Left side of hinder portion of skull of S¢ruthiosawrus austriacus (drawn
reversed for comparison with fig. 7), showing downward direction of
occipital condyle, foramina at base of skull, plate in front of the sella
turcica, transverse groove on roof of skull, &e.
. The same skull seen from the front, showing the parieto-frontal suture,
form of the parietal bone, cerebral cavity, form of the basisphenoid
and sella turcica, &e.
. Right side of hinder part of base of skull of Acanthopholis horridus,
Huxley, showing the united basioccipital and basisphenoid bones,
with the line of large nerve-foramina. (Original m Museum of
Practical Geology.)
. Anterior aspect of same specimen, showing posterior plate of sella turcica.
. Dentary bone of right ramus of lower jaw referred to Cratgomus. The
specimen is seen from above, and shows tooth-sockets along the alve-
olar margin.
. External aspect of same specimen, showing the large foramina below the
alveolar margin and above the longitudinal angle.
. Tooth referred to Cratgomus, probably from the lower jaw, showing
cinguloid ridge at the base of the crown; enlarged twice.
. Similar tooth, less worn, showing serrations on the right margin ; en-
larged twice.
. Tooth referred to the upper jaw of Crat@omus, showing bevelled edges,
probably due to wear; enlarged twice.
. External aspect of same specimen ; enlarged twice.
. Tooth probably of the larger species of Crat@omus.
. Anterior aspect of same tooth, showing cinguloid thickening on both
sides of the crown ; enlarged twice.
. Dorsal rib from the right side, referred to Crateomus lepidophorus,
showing articular surfaces.
. Transverse section from the proximal third of the same rib, showing
transverse expansion of the superior plate and Jateral compression of
the body of the rib.
. Middle of shaft of left tibia referred to Crateomus lepidophorus, showing
muscular ridges on the fibular aspect and commencement of proximal
expansion.
Proximal portion of right fibula of Crat@omus, showing convex tibial
aspect.
. Tooth referred to Megalesaurus pannoniensis; one and a half times
natural size. [The serrations are not directed upward so much as in
the figure. |
. Anterior aspect of the same tooth, showing limit of the serrations.
. Transverse section of base of same tooth, showing posterior compression.
. Tooth of a Crocodile, with slight lateral ridges and worn crown; en-
larged twice.
. A smaller more compressed and curved Crocodilian tooth, showing one
of the lateral ridges; enlarged twice.
. Claw phalange, probably of Rhadinosaurus.
. Internal surface of first left costal plate of Emys Newmayrt.
14.
ON
FAUNA OF THE GOSAU FORMATION. 70
Puate XXVIII.
Proximal portion of left scapula, showing humeral articulation, pro-
bably referable to Mochlodon Suessiz. [The articular surface is longer
than in the figure. |
. Dermal plate referred to Cratgomus, terminating at each end in a free
spine.
. Another dermal plate, with free spines at the ends and similar tubercles
in the middle portion.
. A dermal plate bearing a horn-like spine, also referred to Cratgomus.
A small scute referred to Crateomus, probably from the ventral region.
. Distal portion of right femur of Ornithomerus gracilis, showing part
of the lateral trochanter on the inner side of the shaft.
. Transverse section of the same bone at the proximal fracture, showing
medullary cavity.
Right postfrontal bone of a Chelonian, seen from above, showing the
cranial scutes, referred to Plewropeltus Suessit.
. Internal aspect of the same specimen, showing postorbital ridge and sur-
faces for union with adjacent bones.
. Proximal end of right fibula of Crocodilus proavus.
. Transverse section of the same bone at the distal fracture.
Puate XXIX.
. Superior aspect of left humerus of Crateomus lepidophorus.
. Inferior aspect of right humerus of the same species.
. Proximal surface of left humerus, showing expansion of the radial
crest.
. Inferior aspect of distal end of a humerus referred to Crat@omus Paw-
lowitschit.
. Transverse fracture of proximal end of the same specimen, showing
medullary cavity.
. Side view of claw-phalange of Crateomus.
Internal aspect of proximal end of left femur of Crocodilus proavus.
. Outline of proximal articular surface of the same specimen.
. Ulna of Crocodilus proavus.
. Proximal articular surface of the same specimen.
. Radius of Crocodilus proavus.
. Distal end of the same bone.
. Proximal end of the same bone.
Pirate XXX.
. Superior surface of parietal bone of a small Dinosaur, probably Moch-
lodon Suessit.
. Side view of an angular truncated dorsal piece of dermal armour of
Cratgomus.
. Posterior aspect of dorsal vertebra of Cratcomus Pawlowitschii, showing
transverse processes and fractured base of the neural spine.
. Left side of eariy caudal vertebra of Crateomus Pawlowitschii. [An
earlier caudal exists with the short caudal rib unankylosed. |
. Left side of dorsal vertebra of a Dinosaur, referred to Crateomus lepido-
phorus.
. Right side of mid cervical vertebra of Crocodilus proavus.
. Anterior aspect of the same vertebra.
. Posterior aspect of dorsal vertebra of Crocodilus proavus.
. Left side of dorsal vertebra of Crocodilus proavus.
. Anterior aspect of lumbar vertebra of Crocodilus proavus.
. Left side of the same vertebra.
. Left side of an early caudal vertebra of Crocodilus proavus.
. Inferior aspect of the same vertebra.
Anterior aspect of the same vertebra.
SeeGes. No. 148. BUN
706
PROF. H. G. SEELEY ON THE REPTILE
Fig. 15. Side view of rib and part of superimposed plate, showing the rib free
Fig.
from the plate at the number 15, and the great expansion of the costal
articulation at the other end. Plewropeltus Suesstt.
16. Right hyoplastral element of Emys Newmayri.
Oo Ot oon fF wWhH +
—
iS) tS
fit
(se)
Puate XXXII.
. Anterior aspect of shaft of right femur of Crateomus Pawlowittschii,
showing the muscular ridges.
. Antero-external aspect of right tibia of Crateomus Pawlowitschit.
. Thin slightly keeled dermal plate, probably lateral, of Crateomus lepi-
dophorus.
. Posterior and inferior aspect of left femur of Crateomus lepidophorus.
The figure 4 is placed opposite the small lateral trochanter.
. Anterior and superior aspect of right femur of Crateomus lepidophorus.
. Posterior and inferior aspect of shaft of left femur of Rhadinosaurus
alcimus. The figure 6 is placed against the lateral trochanter.
. Outline of the proximal fracture of the same bone.
. Antero-inferior aspect of shaft of left humerus referred to Rhadinosau-
rus aleimus.
. Outline of proximal fracture of the same bone.
. Outline of distal fracture of the same bone.
. One of the flat dermal plates of Hoplosaurus ischyrus, showing the
cross-fibre structure.
. Proximal end of a rib of Cratgomus Pawlowittschit, for comparison with
fig. 17, Pl. XXVIT. Compare Bunzel, pl. iii. fig. 5.
. Superior aspect of first costal plate of carapace of a Chelonian, Emys
Neumayri.
Synopsis of the Bones figured in these Plates, arranged under the
Species to whach they are referred.
Mocutopon Surssi (Bunzel),.
Dentary bone, Pl. XXVII. fig. 1; teeth, figs. 2-4; scapula, Pl. XXVIII.
fig. 1; parietal bone, Pl. XXX. fig. 1.
STRUTHIOSAURUS AUSTRIACUS, Bunzel.
Hinder portion of skull, Pl. XXVII. figs. 5, 6.
ACANTHOPHOLIS HorRIDUS, Huxley.
Hinder portion of base of skull, Pl. XXVII. figs, 7, 8.
CraT&omMUus (species uncertain).
Dentary bone, Pl. XXVII. figs. 9, 10; teeth, figs. 11-16.
Cratzomus Pawtowitscui, Seeley.
Femur, Pl. XXXI. fig. 1; tibia, fig. 2; fibula, Pl. XXVII. fig. 20; humerus,
Pl. XXIX. figs. 4,5; dorsal vertebra, Pl. XXX. fig. 3; caudal vertebra, iowa
dorsal rib, Pl. SOO, fig. 12; dermal armour, Pl. XXVIII. figs. 2-4.
CRATHOMUS LEPIDOPHORUs, Seeley.
Femur, Pl. XXXI. figs. 4, 5; tibia, Pl. XXVII. fig. 19; humerus, Pl. XXIX.
figs. 1-3 ; dorsal vertebra, Pl. XXX. fig. 5; dorsal rib, Pl. XXVILI. figs. 17,18;
claw-phalange, Pl. XXIX. fig.6; dermal armour, Pl. XXX. fig. 2, Pl. XXXI.
fig. 3, Pl. XXVIII. fig. 5.
Hopiosaurus 18cuyRus, Seeley.
Dermal scute, Pl. XXXI. fig. 11.
FAUNA OF THE GOSAU FORMATION. 707
MEGALOSAURUS PANNONIENSIS, Seeley.
Tooth, Pl. XXVII. figs. 21-23. :
ORNITHOMERUS GRACILIS, Seeley.
Femur, Pl. XXVIII. figs. 6, 7.
RHADINOSAURUS ALCIMUS, Seeley.
eee Pl. XXXI. figs. 6,7; humerus, figs.8-10; claw-phalange, Pl. XXVII.
fig. 26.
Crocopibus PROAVUS, Seeley.
Vertebre, Pl. XXX. figs. 6-14; femur, Pl. XXIX. figs. 7, 8; fibula, Pl.
XXVIII. figs. 10,11; ulna, Pl. XXIX. figs. 9,10; radius, figs. 11-13; teeth,
figs. 24, 25.
PLEUROPELTUS SuEssil, Seeley.
Postfroxntal bone, Pl. XXVIII. figs. 8,9; rib, Pl. XXX. fig. 15.
Emys Neumayrt, Seeley.
Costal plate, Pl. XXVII. fig. 27; Pl. XXXI. fig. 13; hyoplastral plate,
Pl. XXX. fig. 16.
The species described which are not figured are Doratodon carcharidens,
Binzel, Oligosaurus adelus, Seeley, Argosaurus gracilis, Seeley, and Ornitho-
cheirus Biinzeli, Seeley.
Discussion.
Mr. Hurxe considered Prof. Seeley’s paper a very valuable com-
munication, throwing, as it did, fresh light upon an important group
of fossils the true nature of which had before been but imperfectly
apprehended. So far as he had been able to judge from a cursory
inspection of the fossils, he did not doubt the accuracy of Prof.
Seeley’s interpretations. He called attention to the anterior extre-
mity of the mandible of Mochlodon, which had sutural indications of
a preedentary ossification, such as he thought he had seen in Hypsilo-
phodon ; and he mentioned the difficulty which the downward exten-
sion of the Dinosaurian inner trochanter appeared to him to offer
to the hypothesis of its homology with the human trochanter minor,
an extension which suggested that it might rather be homologous
with an outgrowth of the middle part of the linea aspera to which
the short head of the biceps is attached.
Mr. Cuar.LeswortH remarked on the difference between the teeth
in the upper and lower jaw of Mochlodon.
Dr. Murti pointed out that the work of Prof. Seeley showed that
much caution must be exercised in accepting hurried descriptions of
genera and species from fragments,
Prof. Boyp Dawxrns stated that his examination of the American
collections of Secondary Saurians proved that the so-called Megalo-
saurian type of teeth was exhibited by forms belonging to very
different genera. :
The AurHor agreed with Prof. Dawkins’s views concerning the
Megalosaurian teeth, and agreed that teeth were not sufficient alone
. for generic determinations.
3A 2
708 ON A CETACEAN FROM THE LOWER OLIGOCENE OF HAMPSHIRE.
*
43. On the Occurrence of the Remains of a Curacnan in the Lowzr
OxieocrenE Strata of the Hampsuire Basin. By Prof. Jonn W.
Jupp, F.R.S., Sec. G.S.; with an Apprnpix by Prof. SuEtzy,
FE.R.S., F.G.8. (Read June 22, 1881.)
Remains of the marine mammalia have been so seldom recorded
from the Lower Tertiaries of Britain, that the discovery of a new
form is of considerable interest to the geologist. Up to the present
time the only species noticed was the Zeuglodon Wanklyni, described
by Prof. Seeley* in 1876. The remains of this species, which were
found in the Barton Clay, would appear to have been unfortunately
lost. ‘The form which I have now the honour of laying before the
Society is represented by a caudal vertebra only ; but this appears to
present some very interesting peculiarities.
The locality from which this specimen was obtained is Roydon,
about a mile and a half south of Brockenhurst, in the New Forest.
The brickyard at this place is almost the only locality in the New
Forest at which the very interesting marine fauna of the Brockenhurst
Series can now be collected. The beds exposed at this brickyard
consist of sandy clays crowded with marine fossils ; they have been
exposed to the depth of 25 feet ; but as no overlying freshwater beds
have been seen in conjunction with them, the total thickness of the
Brockenhurst Series cannot be determined. Judging, however, from
the wide area over which the beds of this age have been found to
be exposed, that thickness must be considerable. These thick
marine strata are seen at Roydon to rest directly upon freshwater
clays of a bright green colour and crowded with specimens of Unio
Solandri, Sow., which doubtless belong to the Headon Series.
That the Roydon beds belong to the same great marine series as
the beds of Brockenhurst and Lyndhurst appears to be clearly
proved by a comparison of the abundant fossils from the three lo-
calities. On this point Von Konen and the late Mr. F. Edwards,
who collected so assiduously at all those places, appear to have en-
tertained no doubt whatever. Recently, however, an attempt has
been made to separate the Roydon beds into two formations, and
to assign each of these and the Brockenhurst beds to different
geological horizons‘, on the ground that certain forms which are
rare at one locality are abundant at the others, and wice versd.
The fauna of all these beds is so unmistakably that of the Lower
Oligocene or Tongrian that it is impossible to find any valid grounds
for such a subdivision.
Terrestrial mammalia are so abundant in the overlying Bem-
bridge beds, as well as in the underlying Headons, that the disco-
very of this marine form in the Brockenhurst Series is of much
* Quart. Journ. Geol. Soc. vol. xxxii. p. 428, 1876.
Tt Quart. Journ. Geol. Soc. vol. xxxvi. p. 113.
mr
= oe
=
a eee ey es ae eS ee a ee
ee ot
ON THE CAUDAL VERTEBRA OF A CETACEAN, 709
interest, affording, as it does, such an important confirmation of the
ection that a great change i in the physical conditions of the area
must have pecurned at the time when these marine strata were
deposited.
APPENDIX.
Note on the Cavpat VurrEesra of a Curacean discovered by Prof.
Jupp im the Brocxenuurst beds, indicative of a NEw TyPE allied
to BALZNoPTERA (BaL#nopreRs JUDD). By Prof. H. G. Szexey,
RSs GS.
Tuer yertebra submitted to me by Professor Judd belongs to the
caudal region ; and although in a new type there may he some doubt
concerning the exact place in the series, it may be affirmed to have
been about the eighth caudal, and certainly not later than the
twelfth. ‘The vertebra is probably distinct from all recent and
fossil genera; but its characters are altogether in harmony with the
Baleenide ; and the specimen indicates a genus much more closely re-
lated to Balenoptera than to Balena, so far as can be judged from
a single vertebra. This affinity is especially shown in the character
of the base of the centrum, which had the facets for the chevron
bones very small, and also in the general character of the neural
arch, which is much less massive than in Balena. The differences
from the great Balenoptera musculus on the other hand are clearly de-
fined, and appear to consist in the remarkably forward position of the
neural arch (fig. 2), sicein Balenoptera it does not usually reach the
anterior sutural margin. The depressed transversely ovate outline of
the neural canal (fig.3)is another distinctive character, since in Bale-
noptera the neural canal is higher than wide. The neural spine also
appears to be much less developed than in the recent genus, though,
as the hinder part of the neural arch is broken away, this character
cannot be positively affirmed. The centrum is relatively much shorter
(fig. 2); the facets and ridges on the base connected with the chevron
bones are less developed. The transverse width of the zygapophyses
was relatively greater in the fossil. The transverse process is re-
markable for extending the entire width of the centrum (fig. 2), and
for having the vertical perforation rather behind the middle of the
centrum (fig. 1), since in Balenoptera it is placed further forward.
Balenoptera laticeps, however, a species of the North Sea, ranging,
perhaps, to Java and Japan, approaches nearer to the fossil, espe-
cially in having the epiphyses separate; the neural arch, too, is
placed almost as far forward as in the fossil, but is higher, and the
neural spine is larger; but otherwise its characters are very similar.
Perhaps when we reflect that the contemporaries of this old whale
were Palewothzrium, Anoplotherium, and their allies and congeners,
all of which have passed away, it will not seem improbable that the
marine mammals also should give evidence of subgeneric differences.
710 PROF. H. G. SEELEY ON THE CAUDAL VERTEBRA
Fig. 1.— Caudal Vertebra of Balenoptera Juddi, seen from above.
Anterior border.
Posterior border.
{The vertebra does not lean forward as represented in the figure. |
Fig. 2.—Right side of eighth (?) Caudal Vertebra of Balenoptera
Juddi, showing anterior position of the neural arch and vertical
perforation of the transverse process.
i,
i
My,
4,
OF A CETACEAN FROM THE BROCKENHURST BEDS. Flat
Fig. 3.—Anterior Aspect of Caudal Vertebre of Balenoptera Juddi,
showing the depressed form of the neural arch and sutural sur-
face, from which the vertebral epiphysis has come away.
A tail vertebra of a whale, however, is about the last thing which an
anatomist would select to furnish characters for a new genus. I have
not thought that attention is more likely to be called to the fossil by
thus dealing with it than would be the case by adopting the safer
course of shrinking from the responsibility of indicating a genus
which could not at present be sustained.
The centrum has lost its epiphyses (fig. 3); each end is hexagonal,
and marked with the usual radiating longitudinal rugosities. The
centrum is longer at the superior margin, which measures nearly
7 centim., than at the inferior margin, where the measurement is
6:2 centim.; so that there is a conspicuous leaning forward of the
superior margin of the vertebra (fig. 2). - Among vertebrates this cha-
racter recalls a characteristic condition of the vertebrae of Pliosaurus.
As already remarked, the face of the centrum is hexagonal; it is
10-2 centim. wide, and 8-7 centim. deep. ‘The superior surface of the
centrum is short, since the transverse outside measurement of the
neural arch is only 4 centim.; and the width of the base of the cen-
trum is probably no more, though its anterior and posterior margins
are abraded, so that the exact characters cannot be stated. The lateral
surfaces are unequally divided by the transverse processes (fig. 3),
the superior pair, 5°3 centim. long, being the longest. Their mar-
gins are moderately convex ; the inferior lateral borders were under
5 centim. long. The posterior surface of the centrum is broken on
the superior, inferior, and left lateral margins. The lateral margins
AMD ON THE CAUDAL VERTEBRA OF A CETACEAN.
appear to have been more convex behind than in front, and the
transverse width of the centrum appears to have been greater, about
10°6 centim. The base of the centrum is narrow, with a median
longitudinal depression more marked beneath than in front, but
not very conspicuous, and yet sufficient to give the base the appear-
ance of being formed of two rounded lateral portions. The basal
surface is concave from front to back: it is impossible to state its
trausverse width in the middle, because there are no lateral limiting
lines ; but it exceeds 25 centim. ‘The inferior lateral surfaces are
nearly flat from above downward, the concavity being scarcely ap-
preciable, but are markedly concave from front to back. The supe-
rior lateral surfaces are convex from above downwards (fig. 2), the
convexity being least marked in the middle and more marked on the
posterior border than on the anterior border. The length of the
transverse processes cannot be given, because they are fractured ; but
since the fractured end is only half a centim. thick, and 4:7 centim.
wide, it was presumably short. This process is perforated vertically
by an oval foramen (fig.1) which is 7 millim. long and 5 millim. wide.
Its anterior margin is distant 3:4 centim. from the anterior border
of. the vertebra ; and the posterior margin is 2°5 centim. from the
posterior border. On the left side the foramen appears to bea little
smaller, and nearer to the middle of the centrum.
The neural arch is small, depressed, placed anteriorly so as somewhat
to overhang the centrum (fig. 1). It has a scarcely appreciable neural
spine(fig.2); butits posterior margin is broken away. The sides of the ©
neural arch conyerge posteriorly, so that the transverse measurement
behind, as preserved, is 3 centim. The antero-posterior measurement
of the base of the neural arch is rather more than 4 centim. (fig. 2).
The anterior zygapophyses, if such existed, are broken away; and the
extreme transverse width of the neural arch in front (fig. 3), which is
obviously less than its width when perfect, is about 5 centim. ‘The
sides of the arch are directed upward and outward ; and the neur-
apophyses are compressed. The canal for the spinal cord is wider in
front than behind, and higher behind than in front. The transverse
measurement in front is 2°7 centim. The height in front is 1:4
centim. The height behind is about 1:6, as preserved, and the width
fully 2 centim. The neural canal is concave from front to back,
and contains several nutritive foramina. Two are placed near
to the anterior margin, and one in the middle line behind the
middle of the centrum. The superior surface of the neural arch was
probably notched in front, where it was concave from side to side ;
it was inclined backward, where the sides converge, and where it is
divided mesially by the faint indication of a neural spine (fig. 1).
&. H. HOLLINGWORTH ON A PEAT BED AT OLDHAM. FAS.
44. Description of a Prat Bev interstratified with the Bov.pER-
Drirt at OrpHam. By Geo. H. Hotiineworrs, Esq., F.G.S.
(Read June 22, 1881.)
In the early part of September last Mr. James Nield, of Oldham,
called my attention to a bed of peat which he had discovered on the
site of the railway-extensions then being made by the London and
North-Western Railway Co., at Rhodes Bank, Oldham.
The length of the section exposed to view was 53 feet in a north-
to-south direction, and the maximum depth 14 feet; but the depth
of the drift, as proved at the colliery about 100 yards to the west,
is 344 feet.
Section of Boulder-clay with interstratified Peat, near Rhodes Bank,
Oldham. (Scale about 14 feet to 1 inch.)
N. ae
&
SUS Sees
SSe
aie ieee
ee ate, "08 ee
e ies Ee a Sh Reb Sane Manet crea nm reer a .
oe ty hepa) ee Goa —— = > a en F450 Se Se TS ee
mee : S x a? . 9: : ao ene . . >
Pe a Oa 2S patocls Ages Aes A EN noe fae ee, £ o g ole.
. . a ee . K co s - e =
ONC Ie ne On Nan) ga Qi ieee (Vidar wn Sitar On ala. A" a.7 2). 0S VZo Sy
Gray io ao RG! Ae Tae a ies ER toe &-0 962% a DO Sees ay of =
Cele omeyn et <2 S79) Silo Ao 8 4 atin See CNOA Ca po eres aed
° ai) 5 ea ae - Bie . °
Dix anon fo} tescve Y Sean = See a02: S.2% Ge ay vs cftec ROY > fe “9 Co 2 =o cy ts) 9 . =~
es TOR MOR ae O14) Oe eles fel fal ann ISS OA! Kye SIC Soa S26 Ae NSO - ec Ses
= ania S OE) Cheat. crala oa Sen pT eOLD ee oe — °
: "0 J -. ° 2 > pa 5 ec ont BID Sars . °o_ ogo - seenreh*) Cr awe
Pe Sete SO a SE ie eNOS On OI NO CP Scio Ere GoM ec i Bic
° 5
a. Soil. 6. Boulder-clay. c. Fine blue clay.
d. Peat. e. Sand. f. Ochre.
The following is the description of the beds, proceeding down-
wards :—
No.
il SGU scope eanee ee eae ee BREE Ce OTS CREO eee 8 to 10 in.
2. Boulder-clay, sometimes sandy, with beds and | . :
2 to 6 ft.
BUREN DORO ADEA ey esac tasctsa ssdevnserceesSeaeea duane s «
3. Main bed of peat containing mosses, exogenous
stems, and beetles. At one point there was en- | 2 in. to 1 ft. 9 in.
closed in the peat a deposit of iron ochre (f) about { Average 15 in.
6 inches in maximum thickness and 6 feet long...
4. Blue clay, mostly very fine, but stony where] 5 ,, fouleee
thickest, forms the floor clay or soil ...............
5. Current-bedded coarse sand and fine gravel, red- Aen oo ce
BMP EVEMOW-COLOULCH eteer aise. 625 sins wceceae cutee ees
Bee OUIGder-ClAY, LOVED) 5.2 fo< tec. nto dcacecnmecsssnsecens 6 ft.
The deposit is situate in the valley of the Medlock, about 25 feet
above its present level; but it has not beeen exposed by that brook,
at this point, where there is from 2 to 6 feet of the upper clay still
resting upon the peat. The upper clay, peat, and lower clay have
probably been denuded by the action of the brook some yards to the
Q.J.G.S. No. 148. 3B
714 G. H, HOLLINGWORTH ON A PEAT BED AT OLDHAM.
west. The upper clay is continuous to the east for at least 200
yards, and was proved to be about 4 feet thick for 15 yards to the
east of the section by the operations of the Railway Company in
search of sand. At that point the sand was more than 6 feet in
thickness, the bed of peat having run out. The boulders are mostly
from a distance (porphyries, granites, &c.); but a few are of local
origin, one picked up being ganister from the lower coal-measures.
The section, which is now covered up, was measured by me when
about 6 yards of the strata had been excavated from the face at
right angles to the section.
The peat bed terminates on the right of the section; but on the
left or north the upper bed is going forward. ‘The floor clay (4) is
of a fine silty nature generally, and is very similar to the floor clay
of the Ashton Moss (Ashton-under-Lyne) as exposed in the railway-
cutting.
The mosses &c. have been placed in the hands of the Rev. J.
Ferguson, of Brechin, N. B., for examination ; but his final report has
not yet been received. They are, however, of decidedly northern
character.
eal
GENERAL INDEX
TO
THE QUARTERLY JOURNAL
AND
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
[The fossils referred to are described ; and those of which the names are printed
in italics are also figured. |
Abbey Town, section through, 296.
Aberaeron, section from Llandeilo to,
158.
Aberffraw Sands, coast section from
Porth Nobla to, 216.
Aberystwith, constitution of grit from,
8, 25; section from, to the Devil’s
Bridge, 143; section from, through
Pont Erwyd to near Builth, 158;
vertical section of Silurian rocks at,
164.
— grits, 144, 149, 164.
Abnormal geological deposits, Mr. C.
Moore on, in the Bristol district,
67.
Acanthograptus ramosus, 174.
Acanthopholis horridus, 634.
Adriosaurus Suessti, 55.
eee Jelinus, Prof. Owen on,
61
Adolian Sands, 19.
Aitheotesta devonica, 306.
Africa, South, Mr. Dunn on the Dia-
mond-fields of, 609.
African Desert, sand of the, 19.
Age of Archzan rocks of Anglesey,
229.
Alderley Edge, cupreous sandstones
of, 15.
Alum Bay, sands from, 18.
Amaltheus subspinatus, 605.
Amlwch, contorted rocks near, 223;
slates, 223; structure of slaty rock
from near, 235.
Ammonites, Prof. Buckman, on the
terminations of some, from the In-
ferior Oolitesof Dorsetand Somerset,
Ammonites, Mr. 8. 8. Buckman on
some, from the Inferior Oolite of
Dorset, 588.
Ammonites boscensis, 65.
Braikenridgii, 61.
— Brongniarti, 64.
cadomensis, 607.
— concavus, 60.
—— Edouardianus, 61.
— Gervillii, 63.
—— Humphriesianus, 64.
linguiferus, 62.
—— Manselii, 64.
— Martinsii, 63.
—— Moorei, 65.
Sauzei, 62,
—-- subcostatus, 63.
subradiatus, 61.
Analysis of chloritic rock and talcose
schist from Plas Goch, 45, note; of
serpentine from Ty Newydd, 46,
note; of iron-ore from Rio Tinto, 4.
Andesite or basalt from Skomer Is-
land, 411.
Andrews, Rev. W. R., note on the
strata of the Purbeck Beds of the
vale of Wardour, 248.
Anglesey, age of Archean rocks of,
229.
——, Mr. C. Callaway on the Archean
geology of, 210.
——, Prof. T. G. Bonney ona boulder
of Hornblende Picrite near Pen-y-
Carnisiog, 137.
716
Anglesey, Prof. T. G. Bonney on the
microscopic structure of some rocks
from, 282.
Anniversary Address of the President,
Proc. 37. See also Htheridge, R.,
Esq.
Annual Report for 1880, Proce. 8.
Anodontacantius, Mr. J. W. Davis on,
427.
Anodontacanthus acutus, 428.
fastigiatus, 428.
obtusus, 428.
Anomodont reptile (Platypodosaurus
robustus), Prof. Owen on the skeleton
of an: Part II. Pelvis, 266.
Antedon tmpressa, 135.
Arabia Petrza, sand from, 19.
Arzosaurus gracilis, 700.
Archean geology of Anglesey, Mr. C.
Callaway on the, 210.
Archeopteris sp., 305.
Ardennes, Upper Jurassic rocks of
the, 501.
Arenig-felstone and Hskdale-granite
dispersions, junction of the, 361.
Armangon, map of the valley of the,
Ascodictya and Stomatopore. Mr.
Vine on, 613.
Ascodictyon stellatum, 618.
radians, 618.
Ashdown Sands, constitution of, 16.
Ashton, vein at, 77.
Assynt and Durness, Mr. C. Callaway
on the Limestone of, 239.
Asteropteris noveboracensis, 299, 307.
Astroconia Granti, Mr. W. J. Sollas
on, anew Lyssakine Hexactinellid
from the Silurian formation of
Canada, 254.
Athabasea river, British Columbia,
276.
Aube, Upper Jurassic rocks of the,
525 ; map of the valley of the, 526.
Augill, near Brough, Sandstone from,
12
Aust, near Bristol, Mr. J. W. Davis
on the Fish-remains of the Bone-
bed at, 414.
Australia, Devonian plant from, 306.
Auxerre, map of the Yonne valley
south of, 534.
Avon, view of the gorge of the, near
Clifton, 76; Conglomerates of the
gorge of the, 76.
Bagilt, Flintshire, Glacial sands from,
19.
Balenoptera Juddi, 709.
Barmouth, Cambrian Grits of, 7, 25.
Barrah Hill, Section through, 194.
GENERAL INDEX.
Barrois, Dr. C., Award of the Bigsby
Medal to, Proce. 32.
Basalt or Andesite from Skomer Is-
land, 411.
Bay de Chaleurs, Devonian plants
from, 307.
Beddgelert and Snowdon, Mr. F.
Rutley on devitrified rocks from,
——, devitrified spherulitic rock from,
03
Benches in British Columbia, 274.
Bigsby Medal, Award of the, to Dr.
C. Barrois, Proc. 32.
Blake, Rev. J. F., on the correlation
of the Upper Jurassic rocks of
England with those of the Continent,
497.
Bluen y ciel, section through, 159.
Bodafon Mountain, gneissic rocks of,
219.
——, quartz-schist from summit of,
233.
Bodorgan, section on the railway from
Ty Croes to, 217.
——, structure of igneous rock from
a green shale near, 236.
Bodwrog, structure of
limestone from near, 236.
Bolonian of the Boulonnais and HEng-
land, 581.
Bone-bed, Mr. J. W. Davis on the
fish-remains of the, at Aust, near
Bristol.
Bonney, Prof. T. G., on a boulder of
hornblende picrite near Pen-y-
Carnisiog, Anglesey, 137.
, on the microscopic structure of
some Anglesey rocks, 233.
——, on the serpentine and associated
rocks of Anglesey, with a note on
the so-called serpentine of Porth-
dinlleyn (Caernarvonshire), 40.
Bootle bore-hole,constitution of Bunter
sandstone from, 13.
Borth Saint, structure of quartz-schist
from, 233.
Boulder of Hornblende Picrite near
Pen-y-Carnisiog, Anglesey, Prof. T.
G. Bonney on a, 137.
Boulder-clay of West Cumberland and
North Lancashire, 29.
Boulder-drift, Mr. Hollingworth on a
peat-bed interstratified with the,
713.
Boulders, position of, in the Moel-
Tryfan deposits, 354; position of,
in Frondeg gravel-pits, 360.
Boulonnais, Upper Jurassic rocks
of the, 557; map of part of the,
559.
crystalline
GENERAL INDEX.
Bourges, map of country round, 540,
Bovey Heathfield, sands from, 19.
Bradford, constitution of Sandstone
from Spinkwell Quarry near, 11.
Bradford Abbas, vertical section of
Inferior Oolite at, 590.
Braich, section of drift-deposits be-
tween, and the summit of the Ridge,
Frondeg, Denbighshire, 367.
Brampton, section from the Solway to
near, 296.
Brigham, Sandstone from, constitution
of, 11; analysis of, 21.
Bristol district, Mr. C. Moore on ab-
poseal geological deposits in the,
Bristol Reptilia, age of the, 80.
British Columbia, Dr. G. Dawson on
the superficial geology of, 272.
Brockenhurst fauna, affinities of the,
110; relation of Colwell marine
fauna to, 112. ;
Brockenhurst zone at Whitecliff Bay -
and in the New Forest, 109; fossils
of the, 115.
Brodie, Rev. P. B., on certain quartzite
and sandstone fossiliferous pebbles
in the Drift in Warwickshire, and
their probable identity, lthologi-
cally and zoologically, with the true
Lower-Silurian pebbles with similar
fossils in the Trias at Budleigh Sal-
terton, Devonshire, 430.
Bryn-y-Carnau quarry, fossils from.
145.
Bryozoa, fossil Chilostomatous, from
South-west Victoria, Mr. A. W.
Waters on, 309.
Buckman, J., Hsq., on the terminations
of some Ammonites from the Infe-
rior Oolite of Dorset and Somerset,
57.
Buckman, S. S., Esq., on some species
of Ammonites from the Inferior
Oolite of Dorset, 588.
Budleigh Salterton, Lower-Silurian
pebbles in the Trias at, 430.
Bunter sandstones, constitution of, 12.
Caberea rudis, 322.
Caernaryonshire, high-level gravel and
sand in, 357.
Caerwen Farm, section through, 159.
Callaway, Dr. C., on the Archeean geo-
logy of Anglesey, 210.
, on the limestone of Durness and
Assynt, 239.
Calyptograptus digitatus, 174.
plumosus, 173,
Cambrian grits and sandstones, 7.
Canada, Prof. W. J. Sollas on Astvo-
717
conia Granti from the Silurian for-
mation of, 254.
Canda fossilis, 322.
Caradoc Waterfall and Traws Coed,
section in railway-cutting between,
Gy
Carboniferous Fenestellidz, Mr. G.
Shrubsole on the, 178.
grits and sandstones, 11, 25.
Cardigan, 162.
Cardiganshire, South-west, vertical
section of Silurian rocks in, 164.
Cardiopteris ertana, 305.
Cardita-Beaumonti beds of Sind, 193 ;
corals of the, 197.
Carlisle Basin, Mr. T. V. Holmes on
the Permian, Triassic, and Liassic
rocks of the, 286.
Carpenter, P. H., Hsq., on two new
Crinoids from the Upper Chalk of
Southern Sweden, 128.
Carrall, J. W., Esq., on the locality of
some fossils found in the Carboni-
ferous rocks at T’ang Shan, China,83.
Carreg-winllan, structure of igneous
rock from, 236.
Carruthers, W., Esq,, identification of
plants in brown iron-ore from Rio
Tinto, 4.
Carstone, of Hunstanton, constitution
of, 17; analysis of, 18.
Cas Clock, characters of chlorite-
schists from, 234.
Catenicella alata, 317.
ampla, 317.
cribriformis, 317.
elegans, 317.
flexuosa, 317.
— mternodia, 318.
—— marginata, 317.
solida, 318.
Caulopteris Lockwoodi, 307.
Cefn Coch, fossils from, 152.
Hendre, fossils from, 145.
Cellaria fistulosa, 319.
globulosa, 321.
malvinensis, 321.
ovicellosa, 321.
Cellepora fossa, 343.
yarraensis, 343.
sp., d44.
Celluloxylon primevum, 302.
Cemmaes, structure of crystalline
limestone from near, 236.
limestones, 223.
Central Wales, Mr. W. Keeping on
the geology of, 141.
Central zone of Anglesey, 218.
Cerrig Ceimwen, slaty group of, 215;
structure of slaty rock from near,
234,
>
718 GENERAL INDEX.
Cerrig ddwyffordd, structure of slaty
rock from, 234, 235.
Ceryg Moelion, serpentine near, 42 ;
section of quarry at, 43; micro-
scopic character of rock from, 46.
Cetacean, Prof. Judd on the remains
of a, in the Lower Oligocene strata
of the Hampshire basin, 708.
Chalk, Upper, of Southern Sweden,
Mr. P. H. Carpenter on two new
Crinoids from the, 128.
Charente, Upper Jurassic rocks of the,
541.
Charmouth, Mr. Sollas on a new
species of Plesiosawrus from the
Lower Lias of, 440.
Cher, Upper Jurassic rocks of the,
538.
Cheshire, Bunter sandstones of, 12.
Chilostomatous Bryozoa from South-
west Victoria, Mr. A. W. Waters on
fossil, 309.
Chlorite schists of Anglesey, Prof,
Bonney on the, 234.
Chloritic marl and Upper Greensand,
Isle of Wight, Mr. Parkinson on,
370.
schists of Mynydd Mechell, 222.
Cladodus curtus, 422.
Cladophora, Mr. C. Lapworth on the,
in the Llandovery rocks of Mid
Wales, 171.
Clevedon, 78.
Cliff End, Osborne beds at, 104.
Clifton, Rhetic bone-bed near, 75;
view of the gorge of the Avon near,
76.
Clogwyn dur Arddu, devitrified ob-
sidian or rhyolite from, 405.
Clwydd valley, vertical section of Si-
lurian rocks in, 164.
Coal-measures, Mr. J. W. Davis on
Anodontacanthus, a new genus of
fossil fishes from the, 427.
Coal-measure sandstone, from Spink-
nell Quarry, near Bradford, consti-
tution of, 11 ; analysis of, 21; from
Stonyhough, constitution of, 11.
Coast of British Columbia, 277 ; map
of the, 278.
Columbia, British, Dr. G. Dawson on
the superficial geology of, 272.
Colwell Bay, Mr. H. Keeping and Mr.
H. B. Tawney on the beds at Hea-
don Hill and, in the Isle of Wight,
85.
, Lower Headon of, 101; Middle
Headon of, 101.
Colwell marine fauna, relation of, to
the Brockenhurst fauna, 112.
Colwyn Bay, Middle Glacial drift of,
19.
Comén, Prof. Seeley on the remains of
a small Lizard from the Neocomian
rocks of, 52.
Conglomerates of the gorge of the
Avon, 76.
Constitution of grits and sandstones,
Mr. J. A. Phillips on the, 6.
Contortions in railway-cutting near
Traws Coed, 155.
Coppinger, Dr. R. W., on Soilcap-mo-
tion, 348.
Corallian of the Paris basin and Eng-
land, 570.
Coralliferous series of Sind, Prof. P.
M. Duncan on the, 190.
Corals of Sind, 197.
Corris area, 162.
Corwen, N. Wales, Dr. Hicks on some
remains of plants in the Denbigh-
shire grits at, 48.
, section from Nant Llechos, near,
to Moel Morfydd, 487.
Cosmoceras Caumontii, 600.
Garantianum, 600.
Parkinsoni, 599.
subfurcatum, 600.
Craig fawr, 215.
Craig Lluest, section through, 148.
Crateomus, 637.
lepidophorus, 660.
Pawlowitschii, 642.
Cretaceous sandstones, constitution of,
16.
Cribrillina dentipora, 326.
suggerens, 327.
terminata, 326.
Crinoids, Mr. P. H. Carpenter on two
new, from the Upper Chalk of
Southern Sweden, 128.
Crocodilus proavus, 685.
Crogan goch, character of chlorite
schist from, 234.
Crossgates, interglacial deposits at,
33, 37
Cruglas, serpentine near, 42, 45; mi-
croscopic character of, 46.
Ctenoptychius Ordii, 422.
pectinatus, 424.
Cumberland, Mr. J. D. Kendall
on interglacial deposits of West,
29.
Cummersdale, 289.
Cwm, fossils from quarry at, 144.
Cwm Elan, section through, 159.
Cwm Maenydd, 163.
Cwm Symlog, fossils from, 154.
Cwm Ystwyth, section from, to Gwas-
taden, 148.
GENERAL INDEX.
Cyclopteris sp., 305.
Cyclostigma affine, 301.
Dalston, section from Solway Moss to,
296.
Davis, J. W., Esq., on the fish-remains
of the bone-bed at Aust, near Bristol,
with the description of some new
genera and species, 414.
——, on Anodontacanthus, a new
genus of fossil fishes from the coal-
measures, with descriptions of three
new species, 427.
Dawson, Dr. G. M., on the superficial
geology of British Columbia and
adjacent regions, 272.
Dawson, Dr. J. W., award of the
Lyell Medal to, Proc. 30.
——, on new Hrian (Devonian) plants,
299.
Denbighshire grit, constitution of, 9.
——, Dr. Hicks on some plant-re-
mains discovered at the base of the,
Corwen, N. Wales, 482.
Dendroid Graptolites, Mr. C. Lap-
worth on the, in the Llandovery
rocks of Mid Wales, 171.
Depolarization, areas of, from strain
within perlitic bodies in obsidian
tuff, 396.
Devil’s Bridge, section from Aberyst-
wyth to the, 148; fossils from,
147; great inversion of rocks at,
146.
Devitrified rocks, Mr. F. Rutley on,
from Beddgelert and Snowdon,
403.
Devonian grits and sandstones, 9.
plants, Principal Dawson on new,
299.
Diamond-fields of South Africa, Mr.
Dunn on the, 609.
Diastopora, Mr. F. D. Longe on some
specimens of, from the Wenlock
limestone, 239.
Diastopora cricopora, 387.
oolitica, 386.
stomatoporides, 384.
ventricosa, 385.
Diastoporide, Mr. G. R. Vine on the,
from the Lias and Oolite, 381.
Dicranophyllum australicum, 506.
Detyonema corrugatellum, 172.
delicatulum, 172.
venustum, 171.
Dictyophyton, 303.
Dolomitie conglomerate near Clifton,
Doratodon carcharidens, 671.
Dorset, Mr. J. Buckman on some Am-
719
monites from the Inferior Oolite of
Somerset and, 57.
Dorset, Mr. S. S. Buckman on some
Ammonites from the Inferior Oolite
of, 588.
Dovey valley, 162; section through,
163.
Drift-zones, Mr. D. Mackintosh on the
existence of, 351.
Drigg, interglacial deposit at, 34.
Dulas Bay, 220.
Duncan, Prof. P. Martin, presentation
of the Wollaston Medal to, Proc. 28.
, on the coralliferous series of
Sind and its connexion with the
last upheaval of the Himalayas,
190.
Dunn, EH. J., Esqg., on the diamond-
fields of South Africa, 609.
Durdham Down, conglomerate of, 67 ;
section at the edge of, 70; Theco-
dontosawrus-bed of, 73.
Durness and Assynt, Dr. C. Callaway
on the limestone of, 239.
Durness area, map of the, 240.
Dymoke, Keuper sandstone from, 15.
Easton, section through, 296.
Kecles, J., Esq., on the mode of occur-
rence of some volcanic rocks of
Montana, U.S. A., 399.
Egton, constitution of moor grits
from, 16.
Hquisetides Wrightiana, 301.
Emys Newmayrt, 698.
Hppelsheim, 206.
Hrian (Devonian) plants, Principal
Dawson on new, 299.
Erratic stones in the Moel-Tryfan de-
posit, 353.
Eruptive rocks of Skomer Island, Mr.
F. Rutley on, 409.
Etheridge, R., Hsq. (President), Ad-
dress on presenting the Wollaston
Medal to Prof. P. Martin Dunean,
Proc. 28; Address on presenting
the Murchison Medal to Prof.
Archibald Geikie, 29; Address on
handing the Lyell Medal to W. W.
Smyth, Esq., for transmission to
Dr. J. W. Dawson, 30; Address on
handing the Bigsby Medal to Prof.
Morris for transmission to Dr.
Charles Barrois, 32; Address on
handing the Wollaston Donation
Fund to Prof. J. W. Judd for trans-
mission to Dr. R. H. Traquair, 33 ;
Address on presenting the balance
of the Murchison Donation Fund to
Frank Rutley, Esq., 34; Address
720
on presenting one moiety of the
Lyell Geological Fund to G. R.
Vine, Hsq., 35; Address on handing
one moiety of the Lyell Geological
Fund to Prof. H. G. Seeley for
transmission to Dr. Anton Fritsch,
36; Anniversary Address, February
18, 1881. Obituary Notices of De-
ceased Fellows:—Searles Valen-
tine Wood, 37; John Jeremiah
Bigsby, 39; Rev. J. Clifton Ward,
qa) Prot Dy avAnsted, 14:31) Prot
William Hallowes Miller, 44; Mr.
H. Ludlam, 47; Mr. Robert Clut-
terbuck, 48 ; Dr. Edward Meryon,
48; Mr. Elijah Walton, 43 ; Dr. W.
P. Schimper, 49; Dr. J. A. H.
Bosquet, 50; and M. P. H. Nyst,
50. Address on the Analysis and
Distribution of the British Palzo-
zoic Fossils, 51.
Etheridge, R., Esq., on a new species
of Trigonia from the Purbeck beds
of the vale of Wardour, 246.
——, Appendix to Dr. Hicks’s paper
on some plant-remains in North
Wales, 482.
Fault at Porth-y-defaid,
Porth-yr-Ogof, 226.
Felin bont, halleflinta of, 217.
Felsite schist from near Pont-y-Grom-
lech, 405.
Fenestella crassa, 186.
-halkinensis, 187.
—— membranacea, 181.
nodulosa, 183.
—— plebeia, 179.
polyporata, 185.
Fenestellide, Carboniferous, Mr. G.
Shrubsole on the, 178.
Wishes, fossil, Mr. J. W. Davis on
Anodontacanthus, a new genus of,
from the Coal-measures, 427.
Fish-remains of the bone-bed at Aust,
near Bristol, Mr. J. W. Davis on
the, 414.
Flagey gneiss of Durness, 239.
Flintshire, high-level deposits on
Halkin mountain, 357.
Fonthill Giffard, Portlandian sand
from, 16.
Forests, so-called submerged, of West
Cumberland and North Laneashire,
oT.
Fossils, Mr. J. W. Carrall on the
locality of some, m the Carbonife-
rous rocks at T’ang Shan, China.
83.
Fossils of the Middle Headon at Hea-
don Hill and Colwell Bay, 104-106 ;
224; at
GENERAL INDEX.
from the Brockenhurst zone at W hit-
ley Ridge, New Forest, 111; of the
Middle Headon series and Broc-
kenhurst beds,. table of, 115; of
Central Wales, table of, 170; of
the Manchhar series, 204; of the
Upper Greensand and Chloritic
Marl of the Isle of Wight, 371-
373.
Fritsch, Dr. Anton, award of one
moiety of the Lyell Geological
Fund to, Proc. 36. ~
Frodsham, Keuper sands at, 15.
Frondeg gravel-pits, 360; shells
found in, 360; boulders in, 360,
361.
Gaerwen, gneiss of, 212.
Gaj river, section on the north bank
of the, 194.
series, 195; corals of the, 201.
Sipser: River, quartz rhyolite from,
396.
Garthen valley, fossils from, 156.
Geikie, Prof. A., presentation of the
Murchison Medal to, Proc. 29.
Geyser basin, Lower, spherulite rock
from the, 395; vitreous tuff from
the, 396.
Glanrhyd, grey gneiss of, 219.
Gneiss, grey, of the Llangefni area,
218; of Glanrhyd, 219.
Gneissic series of Anglesey, geogra-
phical and stratigraphical distribu-
tion of, 227, 228.
of the Menai anticline, 211;
of the Llangefni syncline, 216;
of the central zone of Anglesey,
219.
Gosau beds of the Neue Welt, Prof.
Suess on the, 702.
formation, Prof. Seeley on the
reptile fauna of the, 620.
Granitoid gneiss, structure of, from
Pen Bryn yr Hglwys, 235.
Granitoidite of Llanerchymedd, 219.
Graptolites, dendroid, Mr. ©. Lap-
worth on the, in the Llandovery
rocks of Mid Wales, 171.
Gravel and sand, arrangement of, in
the Moel-Tryfan deposit, 353 ; high-
level, between Minera and Llan-
gollen vale, Denbighshire, 359;
high-level, near Llangollen, 363;
of Macclesfield forest, 363; high-
level, in Caernarvonshire, 307 ; in
Ireland, 357 ; on Halkin Mountain,
O07.
Great Orton, section through, 296.
Green-quarter Fell,constitution of grit
from, 9.
GENERAL INDEX,
Greensand, Upper, and Chloritic
Marl, Isle of Wight, Mr. Parkinson
on, 370.
Grey gneiss of Glanrhyd, 219; of the
Llangefui area, 218.
Grits, Mr. J. A. Phillips on the con-
stitution and history of, 6.
Gwalchmai, microscopic structure of
quartz- -schists fr om, 232, 233.
Gwastaden, section from Cwm Ystw yth
to, 148; section from Strata Flor ‘ida
and the Teifi pools to, 159.
Gwrthya, 42.”
Gwyn Llyn, section through, 145.
Gypseous shales of Carlisle basin, 288,
295.
Hahn, Dr. Otto, remarks on micro-
scopic sections of meteorites, Proc.
7:
Hala range, 192.
Halkin Mountain, high-level deposits
on, 357.
Halleflinta of the Llangefni area, 217;
near Llangwyllog church, 219.
Hampshire basin, Prof. Judd on the
remains of a Cetacean in the Lower
Oligocene strata of the, 708.
Haploceras oolithicum, 607.
Harpoceras adicrum, 602.
concayum, 603.
cornu, 605.
—— cycloides, 604.
—— dispansum, 604.
—— Hdouardianum, 604.
fissilobatum, 603.
Leyesquei, 604.
— Moorei, 604.
Murchisonez, 603.
Sowerbyi, 602.
Haute-Marne, Upper Jurassic rocks
of the, 516.
Headon beds, list of fossils from the,
105.
—— Hill, Mr. H. Keeping and Mr.
EH. B. Tawney on the beds at, and
at Colwell Bay, Isle of Wight, 85.
, survey section east of, 86;
vertical section at north-east corner
of, 88.
Hempstead series, sands from, 18.
Heppenheim, 206.
Hertfordshire puddingtone, 18.
Hicks, Dr. H., on the discovery of
some remains of plants at the base
of the Denbighshire Grits near
Corwen, North Wales, 482.
High House, sandstone of, 15.
Himalayas, Prof. P. M. Duncan on
the connexion of the Coralliferous
Q. J.G.S. No. 148.
721
series of Sind with the last HE
heaval of the, 190.
Himalayan upheaval, general conside-
rations regarding the age of the
last, 205.
Hollingworth, G. H., Hsq., on a peat
bed interstratified with the boulder-
drift at Oldham, 713.
Holmes, T. V., Esq., on the Permian,
Triassic, and Liassic rocks of the
Carlisle basin, 286.
Holyhead district, 226.
Mountain, quartz-schist from,
226; structure of quartz-schist from,
233.
Holywell, Flintshire,
Boulder-clay at, 19.
Holwell, 67; Postpliocene, Liassic
and Rheetic deposits of, 69.
Hoplosaurus ischyrus, 681.
Hordwell, constitution of sand from,
18.
Hornblende picrite, Prof. T. G. Bon-
ney on a boulder of, near Pen-y-
Carnisiog, Anglesey, 137.
Hunstanton, constitution of Carstone
of, 17; analysis of, 18.
Hybodus austiensis, 416.
punctatus, 417.
sands from
Igneous rocks of Anglesey, Prof. Bon-
ney on the structure of some,
236.
Il-ga-chuz Mountain, British Colum-
bia, 274.
Inchnadamff church,
242.
, plan of limestone and quartzite
at, 243.
Inferior Oolite of Dorset, on some
Ammonites from the, 57, 588.
Interglacial deposits of West Cumber-
land and North Lancashire, Mr. J.
D. Kendall on, 29.
Ireland, high-level gravel and sand
in, 357.
Tron Mountain,
272, 274.
Tron-ore, Mr. J. A. Phillips on the
occurrence of remains of recent
plants in brown, l.
Tron-ores, pisolitic, 18.
Isle of Wight, Mr. Parkinson on the
Upper Greensand and Chloritic Marl
of, 370.
section above,
British Columbia,
Judd, Prof. J. W., on the occurrence
of the remains of a Cetacean in the
Lower Oligocene strata of the
Hampshire basin, with a note by
Prof. Seeley, 708.
3c
722
Jurassic rocks, Upper, of England
and the continent, Rev. J. KF. Blake
on the, 497.
sandstones, constitution of, 16.
Kamloops,
279.
Keeping, H., Esq., and HE. B. Tawney,
Esq., on the beds at Headon Hill and
ee Bay in the Isle of Wight,
Keeping, W., Esq., on the geology of
Central Wales, with an appendix an
some new species of Cladophora by
C. Lapworth, Hsq., 141.
Kendall, J. D., Esq., interglacial de-
posits of West Cumberland and
North Lancashire, 29.
Beran: sandstones, constitution of,
British Columbia, 278,
Khirthar range, geology of the, 193;
diagram section of the, 194.
series, 195; corals of the, 199.
Kimmeridgian of the Paris basin and
England, 577.
Kirklinton sandstone, 290, 295.
La Charité, map of the Loire between
Sancerre and, 538.
Ladock, constitution of grits from, 10.
Laignes, map of part of the valley of
the. 528.
Lake district, vertical section of Silu-
rian rocks in the, 164.
Laki range, geology of the, 193.
Lampeter, fossils from, 155.
Lancashire, Bunter sandstones of, 12.
, Mr. J. D. Kendall on interglacial
deposits of North, 29.
, Mr. T. M. Reade on the date of
the last change of level in, 436.
Lapworth, Prof. C., on the Cladophora
or dendroid Graptolites collected
by Prof. Keeping in the Llandovery
rocks of Mid Wales, 171.
Large-flag series, 151.
Lepidodendron primevum, 302.
Lepralia cleidostoma, var. rotunda,
306.
corrugata, 330.
—— monilifera, 335.
spatulata, 335.
Lias, Mr. Sollas on a new species of
Plesiosaurus in the Lower, Char-
mouth, 440.
in the Carlisle basin, 293, 297.
and oolite, Mr. G. R. Vine on
Diastoporide from the, 381.
Liassic remains, in alluvial veins, in
the Carboniferous of Durdham
Down, 73.
GENERAL INDEX.
Liassic rocks of the Carlisle basin, Mr.
T. V. Holmes on the, 286.
vein in the quarry, Durdham
Down, 75.
Limestone of Durness and Assynt,
Dr. C. Callaway on the, 239.
Limestones, crystalline, of Anglesey,
Prof. Bonney on the structure of,
235.
Lindal, borings in Boulder-clay at,
30, 37.
Lisburne, fossils from, 156.
Litherland, Keuper sandstone from,
15.
Little Orton, section through, 296.
Lizard, Prof. Seeley on the remains of
a small, from the Neocomian rocks
of Comén, near Trieste, 52.
Llanbrynmaer, 161; vertical section of
Silurian rocks at, 164.
Llandeilo, section from, to Aberaeron,
108 ; vertical section of Silurian
rocks west of, 164.
Llandovery rocks of Mid Wales, Mr.
C. Lapworth on the Cladophora of
Ofte isle
Llanerchymedd and Llangwyllog, sec-
tion between, 219.
Llanfadog uchaf, section through, 159.
Llanfechell grits, 223; structure of
slaty rock from, 254.
Llangefni syncline, 213, conglomer-
ates and shales, 214; conglomerate,
structure of a fragment of grit i,
235.
Llangollen, high-level gravel and sand
near, 363.
Llangollen valley and Minera, high-
level deposits between, 359.
Llangrannog, constitution of grit from,
8
Llangristiolus grits and slates, 214.
Llangwrig, section through, 159.
Llangwyllog church, Halleflinta near,
219.
—-— and Llanerchymedd, section be-
tween, 219.
Lianwenllwyfo, 220.
Lian y Mowddwy, vertical section
across the Dovey valley at, 163 ; ver-
tical section of Silurian rocks at, 164.
Loire, map of the, between Sancerre
and La Charité, 538.
Longe, F. D., Esq., on some specimens
of Diastopora and Stomatopora from
the Wenlock limestone, Proc. 239.
Lower Charente, Upper Jurassic rocks
of the 543.
Lower Geyser basin, spherulite rock
from the, 395; vitreous tuff from
the, 396.
2 eae
GENERAL INDEX.
Lower Headon beds, 94; of the cliffs
between Weston and Widdick
Chines, 96; of Warden Cliff, 97 ,
of Colwell Bay, 101.
Lower Lickey Hills, Upper Llando-
very sandstone from, 9.
Lower Mottled Sandstones, 12, 14.
Lower Oligocene strata of the Hamp-
shire basin, Prof. Judd on the re-
mains of a Cetacean in the, 708.
Lower Permian of the Carlisle basin,
287.
Lunulites cancellata, 344.
guineensis, 344.
Lyell Geological Fund, presentation
of one moiety of, to G. R. Vine,
Esq., Proc. 35 ; award of one moiety
of the, to Dr. Anton Fritsch, Proc.
36.
Lyell Medal, award of the, to Dr. J.
W. Dawson, Proc. 30.
Lyssakine Hexactineliid, Prof. W. J.
Sollas on a new, from the Silurian
formation of Canada, 254.
Lytoceras confusum, 601.
—— Hudesianum, 601.
-—— torulosum, 601.
Macclesfield Forest, high-level gravel
and sand of, 363.
Machynlleth, fossils from Morben
quarry, 153.
Mackintosh, Mr. D., on the precise
mode of accumulation and deriva-
tion of the Moel-Tryfan shelly
deposits and similar high-level de-
posits along the eastern slopes of
the Welsh mountains, and on the
existence of drift-zones, showing
probable variations in the rate of
submergence, 351.
Mammalian jaw, Mr. E. W. Wil-
lett on a, from the Purbeck beds at
Swanage, 376.
Manchhar series of Sind, 196; equi-
valence of the, and the Sivalik group
of the Himalayas, 202.
Map of country near Neuvizy, 502;
round Verdun, 507 ; round St. Mi-
hiel, 511; between the Meuse and
Ornain, 514; of part of the valley
of the Rognon, 518; of part of the
Marne valley, 520; of the valley of
the Aube, 526; of part of the val-
ley of the Laignes, 528; of the val-
ley of the Armangon, 551, of the
Yonne valley south of Auxerre, 534 ;
of the Loire valley between San-
cerre and La Charité, 538; of
country round Bourges, 540; of the
coast round the Pertuis d’Antioch,
723
544; of the coast near Trouville,
548; of part of the Pays de Bray,
506; of part of the Boulonnais,
559.
Map of part of British Columbia, 278.
eee part of the Yellowstone Park,
400.
Map of the coast at Blundellsands,
near Liverpool, 436.
Map of the Durness area, 240.
Market Rasen, pisolitic iron-ore from,
18.
Marl, Chloritic, and Upper Green-
sand, of the Isle of Wight, Mr. Par-
kinson on, 370.
Marne valley, map of part of the, 520.
Maryport, interglacial deposit at, 36.
May-hill sandstone, constitution of, 8.
Megalosaurus pannoniensis, 670.
Melin Carnau, 42.
Melin pant y gwyda, structure of
chlorite-schist from, 234.
Membranipora argus, 324.
—— catenularia, 323.
concamerata, 324.
— cylindriformis, 328.
—— geminata, 325.
lineata, 323.
——. lusoria, 324.
—— macrostoma, 323.
maorica, 325.
Menai anticline, 211.
Mesocrinus suedicus, 130.
Metalliferous slate group, 145, 152.
Metalliferous slates, 164.
Meteorites, Dr. Otto Hahn’s remarks
on microscopic sections of, Proc. 7.
Meuse, Upper Jurassic rocks of the, 505.
Meuse and Ornain, map of country
between the, 514.
Micklethwaite, section through, 296.
Microlestes quarry at Holwell, 69.
Micropora patula, 326.
Microporella enigmatica, 331.
clavata, 332.
—— coscinopora, 331.
—— elevata, 330.
—— ferrea, 330.
—— symimetrica, 332.
—- violacea, 329.
yarraensis, 331.
Microscopic characters of volcanic
rocks from Montana, 398.
Microscopic structure of some Angle-
sey rocks, Prof. T. G. Bonney on
the, 233.
Middle Headon beds, 92; of Warden
cliff, 100 ; of Colwell Bay, 101; of
Whitechff Bay, 108.
Millet-seed beds, 12, 26.
Millstone-grit Sandstone, from Brig-
724
ham, constitution of, 11; analysis
of, 21,
Minera and Llangollen, high - level
deposits between, 350.
Mochlodon Suessti, 624.
Moel Morfydd, section from Nant
Llechos, near Corwen, to, 487.
Moel Tryfan, shelly deposits of, 351 ;
deposition of, during submergence,
353; identification of local and
erratic stones in, 353; arrangement
of the gravel and sand in, 353;
position of boulders in, 354; bent
and shattered edges of slaty laminz
in, 854, 368; origin of shells of,
355; section of laminated sand and
bent slates on, 355.
Moel-Tryfan shelly deposits and simi-
lar high-level deposits on the Welsh
mountains, Mr. Mackintosh on the,
Bol,
Montana, U.S. A., Mr. F. Rutley on
the vitreous rocks of, 391.
, Mr. J. Eecles on some volcanic
rocks of, 391.
, microscopic characters of vol-
eanic rocks from, 398.
Moore, C., Esq., on abnormal geologi-
cal deposits in the Bristol district,
67.
Morben quarry, Machynlleth, fruits
from, 153.
Mucronella duplicata, 328.
elegans, 329.
mucronata, 328.
Murchison Fund, presentation of the
Balance of, to Frank Rutley, Esq.,
Proc. 34.
Murchison Medal, presentation of,
to Prof. Archibald Geikie, Proc.
29.
Mynyda Liwydiarth, gneiss of, 212.
Mynydd Mechell, chloritic schists of,
222.
Nant Cader, section through, 159.
Nant Llechos, near Corwen, section
from, to Moel Morfydd, 487.
Nari series, 195; Corals of, 200.
Nebo, 220.
Nemacanthus minor, 419.
Nematophycus Hicksti, 494.
Neocomian rocks, Prof. Seeley on a
small Lizard from the, of Comén,
near Trieste, 52.
Nettlebury Quarry, 78.
Neue Welt, Prof. Suess on the Gosau
beds of the, 702.
Neuvizy, map of country near, 502.
New Brunswick, plants from the De-
yonian of St. John, 303.
GENERAL INDEX.
nee Forest, Brockenhurst zone in the,
109.
New York, plants from the Devonian
of, 299, 303.
Nicols River, British Columbia, 273.
Niévre, Upper Jurassic rocks of, 537.
Normandy, Upper Jurassic rocks of,
DAT.
Northern area of Anglesey, 221.
North-western area of Anglesey, 224.
Oborne, near Sherborne, vertical sec-
tion of Inferior Odlite at, 589.
Obsidian, devitrified, 405, 411.
Obsidian from the Yellowstone dis-
trict, 392; black, 391; felspar crys-
tals in, 392; black spherulitic, 393 ;
spherulitic-banded, 393 ; black por-
phyritic, 394.
Obsidian from Tolcsva, Hungary, 406.
Obsidian tuff, areas of depolarization
fromstrain in perlitic bodies in, 396.
Odontocaulis Keepingii, 176.
Odontopteris squamosa, 305.
Okanagan valley, British Columbia,
278, 279.
Oldham, Mr. Hollingworth on a peat
bed interstratified with the Boulder-
drift at, '713.
Oligosaurus adelus, 678.
Oolite, Mr. J. Buckman on some Am-
monites from the Inferior, of Dorset
and Somerset, 57.
, Inferior, of Dorset, Mr. S. S.
Buckman on some Ammonites from
the, 588.
and Lias, Mr. G. R. Vine on
Diastoporide from the, 381.
Oolitic remains at Westbury-on-Trym,
(de
Oppelia subcostata, 606.
—— subradiata, 606.
Truellii, 606.
Ormskirk, constitution of Sandstones
from Town Green, near, 14.
Orne and Sarthe, Upper Jurassic rocks
of the, 547.
Ornithocheirus Binzeli, 701.
Ornithomerus gracilis, 671.
Osborne Beds at Cliff End, 104.
Owen, Prof., on the parts of the Ske-
leton of an Anomodont Reptile
(Platypodosaurus robustus, Owen),
Part II. The Pelvis, 266.
, on the Order Therodontia, with
a description of a new genus and
species (Ailurosaurus felinus, Ow.),
261.
Oxfordian of the Paris basin and
England, 567.
Pachytheca, 484, 492.
GENERAL INDEX,
Paleosaurus Stricklandi, 420.
Paris Basin, Rev. J. F. Blake on the
Upper Jurassic of the, +97.
Paris Mountain, area south of, 220;
Mr. Allport on rocks from, 220;
volcanic group of, 221.
Parkhead, sandstone from, 12.
Parkinson, C., Esq., on Upper Green-
sand and Chloritic Marl, Isle of
Wight, 370.
Patagonian archipelago, Soil-cap mo-
tion in the, 348.
Pays de Bray, Upper Jurassic rocks of
the, 554; map of part of the, 556.
Peace River, British Columbia, 276.
Peat-bed interstratified with the
Boulder -drift at Oldham, Mr.
Hollingworth on a, 713.
Pelvis, Prof. Owen on the, of an Ano-
modont Reptile, 266.
Pen bryn’r Eglwys, section from
Porth-y-defaid to, 224; structure of
granitoid gneiss from, 235.
Pen Rhiev Wen, section through, 143.
Penrith Sandstone, 287.
Pentewan, shore-sand from, 19, 25.
Pentraeth, gneiss south of, 211;
structure of crystalline limestone
from near, 235, 236.
Pen-y-Carnisiog, Anglesey, Prof. T. G.
Bonney on a boulder of hornblende
picrite near, 137.
Perisphinctes Martinsii, 601.
pygmeeum, 601.
Permian, Lower, of the Carlisle basin,
287.
Permian, Upper, of the Carlisle Basin,
286.
Permian rocks, of the Carlisle Basin,
Mr. T. V. Holmes on the, 286.
Permian Sandstones, constitution of,
22:
Perranzabuloe, constitution of grit
from, 10,
Pertuis d’Antioch, map of the coast
round the, 544.
Phillips, J. A., Esq., on the occurrence
of remains of recent plants in
brown iron-ore, 1.
, on the constitution and his-
tory of grits and sandstones, 6.
Picrite, hornblende, Prof. T. G.
Bonney on a boulder of, 137.
Pikermi, 206.
Pisolitic iron-ores, 18.
Pian of limestone and quartzite at
Inchnadamff, 245; of part of Rio
Tinto, 3.
Plants, Dr. Hicks on the remains of
some, near Corwen, North Wales,
482.
725
Plasgoch, section in quarry at, 44;
analyses of rocks from, 45, note ;
microscopic character of rock from,
46.
Plastremys lata, 370.
Plas uchaf, 220.
Platypodosaurus robustus, Prot. Owen
on the pelvis of, 266.
Plesiosaurus brachycephalus, 476.
conybeari, 440.
megacephalus, 440.
Pleuropeltus Suessti, 693.
Plynlimmon, vertical section of Silu-
rian rocks at, 164.
grits, 162.
group, 156.
Point Atlianus, structure of slaty rock
from, 235.
Pont Cletwr Yspytty, constitution of
erit from, 9.
Erwyd, fossils from near, 152;
section from, through the Plyn-
limmon axis to Llangwrig and
Rhyader, 159.
Pont ur Elan,
148.
Pont-y-Gromlech, felsite schist from
near, 405.
Popty, section through, 143.
Porella denticulata, 336.
emendata, 336.
Porina clypeata, 332.
columnata, 334.
coronata, 332.
Porthdinlleyn, Prof. Bonney on the
so-called serpentine of (Caernarvon-
shire), 40.
Porth feiin, structure of
schist from, 234.
Porth lygan, 220.
Porth Nobla, coast-section from, to
Aberffraw sands, 216.
Porth-y-defaid fault, 224; section
from, to Pen bryn’r Eglwys, 224;
structure of chlorite-schist from,
234.
Porth-yr-Ogof fault, 226; structure
of chlorite-schist from, 234.
Portlandian of the Paris basin and
England, 585.
Post-Tertiary sands, constitution of,
18).
Psaronius textilis, 307.
Purbeck beds, Mr. R. Etheridge on a
new species of Zrzgonia from the,
of the Vale of Wardour, 246.
Purbeck beds at Swanage, Mr. E. W.
Willett on a mammalian jaw from
the, 376.
section through,
chlorite-
Quartzite and sandstone fossiliferous
726 GENERAL INDEX.
pebbles in the drift in Warwick-
shire, Rey. P. B. Brodie on certain,
430.
Quartzite of Durness, 242.
Quartz rhyolite, from Yellowstone
Canon, 395; from Gardiner’s River,
396.
Quartz-schist from Holyhead Moun-
tain, 226; of the Llangefni area,
PAT
of Anglesey, Prof. Bonney on
the characters of, 232.
Queen-Charlotte Islands, glaciation of
the, 280.
Ranikot series, 193; corals of, 197.
Reade, T. M., Esq., on the date of the
last change of level in Lancashire,
436.
Recent plants in brown iron-ore, Mr.
J. A. Phillips on the occurrence of
remains of, |.
Reptile fauna of the Gosau formation,
Prof. Seeley on the, 620.
Reptilia, age of the Bristol, 80.
Retepora marsupiata, 342.
rimata, 3438.
Rhadinosaurus alcinus, 675.
Rheetic bone-bed near Clifton, 75.
Rheetic remains in alluvial veins in
the Carboniferous of Durdham
Down, 73.
Rheda, Cumberland, constitution of
St.-Bees sandstone of, 12.
Rhodes Bank, Oldham, section of
boulder-clay with interstratified
peat near, 713.
Rhosbeirio shales, 225.
Rhoscolyn, serpentine from near, 40,
42.
church, quartz-schist from, 233.
district, contortiou of rocks in,
227.
Rhyader, section through, 143; sec-
tion from Pont Erwyd through the
Plynlimmon axis to Llangwrig and,
159; vertical section of Silurian
rocks at, 164.
Rhyolite, quartz,
River, 396;
Canon, 395.
from Clogwyn @ur Arddu, 405.
Rio Tinto, remains of recent plants in
brown iron-ore at, 1.
, plan and section of part of, 3.
, analysis of iron-ore from, 4.
Rocks, Anglesey, Prot. 'T. G. Bonney
on some, 232.
, devitrified, Mr. F. Rutley on,
from Beddgelert and Snowdon,
405.
from Gardiner’s
from Yellowstone
Rocks, eruptive, Mr. F. Rutley on the,
of Skomer Island, 409.
, Serpentine and associated, Prof.
Bonney on the, of Anglesey, 40.
, vitreous, Mr. F. Rutley on the,
of Montana, U.S. A., 391.
, volcanic, Mr. Hecles on some,
of Montana, U.S. A., 399.
Rognon, map of part of the valley of
the, 518.
Roydon brickyard, section in, 113,
note.
zone, 113.
Runcorn station, constitution of sand-
stone from, 15.
Rutley, Frank, Esq., presentation of
the balance of the Murchison Fund
to; Proes 3a.
, on the microscopic characters
of the vitreous rocks of Mon-
tana, U.S. A., with an appendix by
Mr. J. Eccles, 391.
, on the microscopic structure of
devitrified rocks from Beddgelert
and Snowdon, with an appendix on
the eruptive rocks of Skomer Island,
403.
Beare constitution of grit from,
0.
St. Austell, constitution of grits from
near, 9, 25.
river, sands of, 21.
St. Bees, interglacial deposits at, 35.
sandstone, 286; constitution of,
12.
St. Ewe, constitution of grits from, 9.
St. John, New Brunswick, plants from
the Devonian of, 303.
St. Mihiel, map of country round,
511.
Sancerre, map of the Loire between
La Charité and, 538.
Sands, water-borne, examination of,
21.
Sandstone and quartzite fossiliferous
pebbles in the drift inWarwickshire,
Rev. P. B. Brodie on, 430.
Sandstones, Mr. J. A. Phillips on the
constitution and history of, 6.
Sango Bay, gneiss of, 241.
Sarthe and Orne, Upper Jurassic rocks
of the, 547.
Schist, dark, of the Llangefni area,
218; of Glanrhyd, 219.
Schists of Holyhead island, micro-
scopic characters of, 47.
Schizoporella amphora, 341.
australis, 341.
conservata, 340.
— excubans, 341.
GENERAL INDEX. aL
Schizoporella fenestrata, 339.
phymatopora, 338.
spiroporina, 340.
—— submersa, 340.
—— ventricosa, 338.
—— vigilans, 338.
sp., 339. ;
Scotland, Devonian plant from, 306.
, South, vertical section of Silu-
rian rocks in, | 64.
Sections :—of part of Rio Tinto, 3; of
junction of schist and serpentine,
41; of quarry at Ceryg Moelion,
43; of quarry at Plas Goch, 44;
at the edge of Durdham Down, 70:
of Thecodontosaurus-bed of Durdham
Down, 73; vertical, at north-east
corner of Headon Hill, 91; vertical,
of Lower Headon (freshwater) beds
exposed between Weston Chine and
Warden Cliff, 98; vertical, of Up-
per Headon beds in Colwell Bay,
103; from Aberystwith to the Devil’s
Bridge, 143; from Cwm Ystwyth,
through Craig Lluest, to Rhyader
and Gwastaden, 143; in railway-
cutting between Traws Coed and
Caradoc waterfall, 155; from Pont
Erwyd through the Plynlimmon
axis to Llangwrig and Rhyader,
159; from Strata Florida and the
Teifi pools to Rhyader and Gwas-
taden, 159; showing general struc-
ture of Central Wales, 160; through
the Dovey valley at Llan y Mowd-
dwy, 163; vertical, of Silurian
rocks in the English lake-district,
South Scotland, South-west Cardi-
ganshire, at Rhyader, west of Llan-
deilo, at Aberystwyth and Plynlim-
mon, Llanbrynmaer, and Llan y
Mowddwy, and in the Clwydd val-
ley, 164; through Barrah Hill, 194;
of the Khirthar range, on the north
bank of the Gaj river, 194; above
Inchnadamff church, 242; of Pur-
beck beds in a railway-cutting west of
Dinton Station, Vale of Wardour,
252; from the Solway, north of
Allonby, to near Brampton, 296;
from Solway Moss to Dalston, 296 ;
from Tordoff Point, Dumfriesshire,
to the fault south of Wigton, 296;
of laminated sand and bent slates
on Moel Tryfan, 355; of drift-de-
posits between Braich and the sum-
mit of the ridge, Frondeg, Denbigh-
shire, 367; of Upper Greensand
and chloritic marl, St. Lawrence
and Ventnor, Isle of Wight, 374;
at Blundellsands, near Liverpool,
437; from Nant Llechos, near Cor-
wen, to Moel Morfydd, 487; of
boulder-clay with interstratified
peat, near Rhodes Bank, Oldham,
718.
Seeley, Prof. H. G., on remains of a
small lizard from the Neocomian
rocks of Comén, near Trieste, pre-
served in the Geological Museum of
the University of Vienna, 52.
—, on the reptile fauna of the
Gosau formation, preserved in the
Geological Museum of Vienna, 620.
, on the caudal vertebra of a Ce-
tacean, discovered by Prof. Judd in
the Brockenhurst beds, indicative of
a new type allied to Balenoptera
(Balenoptera Juddi) 709.
Selenaria alata, 344.
marginata, 344.
Serpentine, Prof. Bonney on the so-
called, of Porthdinlleyn (Caernar-
vonshire), 40.
, Prof. Bonney on the, of An-
glesey, 40.
Sevenoaks stone, constitution of, 16.
Shalk Beck, Yoredale grit from, con-
stitution of, 11; analysis of, 21.
Shells, of Moel-Tryfan deposit, origin
of the, 355.
Sherborne, vertical section of Inferior
Oolite at Oborne, near, 589.
Shrubsole, Mr. W., on the Carboni-
ferous Fenestellide, 178.
Silurian grits and sandstones, 7, 25.
formation, Mr. W. J. Sollas on
Astrocoma Granti, from the, of
Canada, 254.
uniserial Stomatoporee and Asco-
dictya, Mr. Vine on, 613.
Sind, Prof. P. M. Duncan on the co-
ralliferous series of, 190.
, Western, Table of formations in,
192.
Sivalik group, equivalence of the
Manchhar series of Sind with the,
202.
Skomer Island, Mr. F. Rutley on the
eruptive rocks of, 409.
Slaty laminz, bent and shattered edges
of, at Moel Tryfan, 354, 368.
rocks of Anglesey, Prof. Bonney
on the structure of, 234.
series of Anglesey, geographical
distribution of, 225.
of the central zone of
Anglesey, 218.
of the Menai anticline, 213;
of the Llangefni syncline, 214.
Smith, Dr. William, presentation of
portrait of, Proc. 2.
——
728
Smittia anceps, 337.
centralis, 337.
, var. levigata, 337.
Tatei, 337.
Snowdon and Beddgelert, Mr. F.
Rutley on devitrified rocks from,
403.
Soilcap-motion, Mr. R. W. Coppinger
on, 348.
Sollas, Prof. W. J., on Astroconia
Granti, a new Lyssakine Hexacti-
nellid from the Silurian formation
of Canada, 254.
—, on a new species of Plesiosaurus
(P. Conybearz) from the Lower Lias
of Charmouth, with observations on
P. megacephalus, Stutchbury, and
P. brachycephalus, Owen, 440.
Solway, section from the, to near
Brampton, 296.
Solway Moss, section from, to Dalston,
295.
Somerset, Mr. J. Buckman, on some
Ammonites from the Interior Oolite
of Dorset and, 57.
South Thompson valley, British Co-
luinbia, 2795.
Spheroceras Brongniarti, 596.
dimorphum, 9598.
—— Gervillii, 597.
—— Mantellii, 597.
—— polymorphum, 598.
Wrightii, 598.
Sphenonchus obtusus, 420.
nt
Spherulitic rock, devitrified, from.
Beddgelert, 403.
from the Lower Geyser
basin, 395.
from the Yellowstone dis-
trict, 394. ;
Spinkwell quarry, constitution of
Coal-measure sandstone from, 11 ;
analysis of, 21.
Spirophyton, 303.
Stanwix, section through, 296.
Stanwix marls, 292, 295.
Stedd fa Gurig, section through, 159.
Stephanoceras Braikenridgii, 595.
Deslongchampsi, 594.
—_— Humphriesianum, 594.
linguiferum, 595.
—— polymerum, 596.
zigzag, 596.
Stiper stone, constitution OI, Uf, UD:
Stomatopora, Mr. F. D. Longe on
some specimens of, from the Wen-
lock limestone, Proc. 239.
Stomatopora dissimilis, 615.
inflata, 615.
Stomatopore and Ascodictya, My.
G. R. Vine on, 615.
GENERAL INDEX,
Stonyhough, constitution of coal-
measure sandstone from, L1.
Stow-on-the-Wold, constitution of
Liassic sand from, 16.
Strata Florida rock, 154.
Struthiosaurus austriacus, 628,
Submerged forests, so-called, of West
Cumberland and North Lancashire,
oT.
Submergence, deposition of Moel-Try-
fan shelly beds during, 353.
——, Mr. D. Mackintosh on drift-
zones and probable variations in the
rate of, 357.
, rate of, in Denbighshire, 362.
Suess, Prof. E., on the Gosau beds of
the Neue Welt, west of Wiener
Neustadt, 702.
_ Superficial geology of British Colum-
bia and adjacent regions, Dr. G.
Dawson on, 272.
Swanage, Mr. H. W. Willett on a
mammalian jaw from the Purbeck
beds at, 376.
Sweden, Mr. P. H. Carpenter on two
new Crinoids from the Upper Chalk
of Southern, 128.
T’ang Shan, Mr. Carrall on some fossils
found in carboniferous rocks at, 83.
Tan y graig, Pentraeth, structure of
crystalline limestone from, 236.
Tau isa, Cemmaes, structure of crys-
talline limestone from, 236.
Tawney, H. B., Esq., and H. Keeping,
Esq., on the beds at Headon Hill and
Colwell Bay in the Isle of Wight,
85.
Teifi pools, section from, to Gwasta-
den, 159,
Terraces in British Columbia, 274.
Tertiary sandstones and grits, consti-
tution of, 18.
Thames valley, sands of the, 19.
Thecodontosaurus-bed of Durdham
Down, 73.
Theriodontia, Prof. Owen on Aluro-
saurus felinus, a new species and
genus of, 261.
Thornbury railway, Secondary veins
on, (9:
Thornby, section through, 296.
Tilgate sandstone, constitution of, 16.
Tolesya, Hungary, deep red obsidian
from, 406.
Tonnerre, map of the valley of the
Armancon, north of, 531.
- Tordoff point, section from, to the
fault south of Wigton, 296.
Town Green, near Ormskirk, consti-
tution of sandstone from, 14.
GENERAL INDEX.
Trachyte, quartz-oligoclase, from Sko-
mer Island, 411.
Traquair, Dr. R. H., award of the
Wollaston Donation Fund to, Proc.
33-
Traws Coed and Caradoc waterfall,
section in railway-cutting between,
155.
Triassic rocks of the Carlisle basin,
Mr. T. V. Holmes on the, 286.
Triassic sandstones, constitution of,
12, 25, 26.
Triconodon mordax, 378.
Trieste, Prof. Seeley on the remains of
a small Lizard from the Neocomian
rocks of Comén, near, 52.
Trigonia, Mr. R. Etheridge on a new
species of, 246.
— densinoda, 246.
Trouville, map of the coast near,
548,
Tubutella ambigua, 71, 80.
Tuff, vitreous, from the Lower Geyser
basin, Yellowstone district, 396.
Ty Croes, section on the railway from,
to Bodorgan, 217 ; structure of rock
from, 233.
Tyddyn Gob, 41, 47.
Ty Newydd, 40; microscopic character
of rock from, 46; analysis of ser-
pentine from, 46, ote.
Ty Ucha, 41; microscopic characters
of rock from, 45.
Upper Greensand, Mr. Parkinson on
the, and chloritic marl, Isle of
Wight, 370.
Upper Headon beds, 92; of Colwell
bay, 102.
Upper Jurassic rocks of England, Rev.
J. HF. Blake on the correlation of the,
with those of the continent, 497.
Upper Mottled Sandstones, 12, 14.
Upper Permian of the Carlisle basin,
286.
Veins, alluvial, with Liassic and Rhx-
tic remains, in the carboniferous of
Durdham Down, 73.
Verdun, map of the country round,
HUM
Vertebra, caudal, of a Cetacean, Prof.
Seeley on the, 709.
Victoria, Mr. A. W. Waters on fossil
Chilostomatous Bryozoa from
South-west, 309.
View of perched gravel-mound on
Halkin Mountain, 358.
Vine, G. R., Esq., presentation of one
moiety of the Lyell Geological Fund
to, Proc. 35.
Q.J.G.8. No. 148.
729
Vine, G. R., Hsq., on the Family Dias-
toporide, Busk:—species from the
Lias and Oolite, 381.
, on Silurian uniserial Stomato-
pore and Ascodictya, 613.
Vitreous rocks, Mr. F. Rutley on, of
Montana, U.S. A., 391.
Voleanie group of Paris Mountain,
=
rocks from Montana, microscopic
characters of, 398.
of Montana, U.S. A., Mr.
Eccles on some, 399.
Wales, Central, diagram of the general
structure of, 160.
; , Mr. W. Keeping on the
geology of, 141.
, North, Dr. Hicks on some
remains of plants in the Denbigh-
shire grits at Corwen, 482.
Walney, interglacial deposit at, 34.
Warden cliff, Lower Headon beds of,
97; Middle Headon beds of, 100.
and Weston chine, verti-
cal section of Lower Headon (fresh-
water) beds exposed between, 98.
Wardour, Mr. R. Etheridge on a new
species of Trigonia from the Pur-
beck beds of the vale of, 246.
Warwickshire, Rev. P. B. Brodie on
quartzite and fossiliferous pebbles
in the drift in, 480.
W ater-borne sands, examination of, 21.
Waters, A. W., Esq., on fossil Chilo-
stomatous Bryozoa from South-west
Victoria, 309.
Waterstone beds, constitution of, 15.
Welsh mountains, Mr. Mackintosh on
Moel-Tryfan shelly deposits and
similar high-level deposits on the,
ool.
Wenlock limestone, Mr. F. D. Longe
on some specimens of Dzastopora
and Stomatopora from the, Proc.
239.
Westbury-on-Trym, carboniferous
limestone with minerals and oolitic
remains, 77.
Western area of Anglesey, 225.
Weston chine, Lower Headon beds of
the cliff between, and Widdick
chine, 96.
and Warden cliff, vertical
section of Lower Headon (fresh-
water) beds exposed between, 98.
Whidborne, G. F., Hsq., on the genus
Plesiosaurus, 440.
Whitecliff bay, Middle Headon of,
108; Brockenhurst zone at, 109.
Widdick chine, Lower Headon beds of
3D
730
the cliffs between, and Weston chine,
96
Wigton, section from Solway Moss to
the fault south of, 296.
Willett, EK. W., Esq., on a mammalian
jaw from the Purbeck beds at
Swanage; with a note by H. Wil-
lett, Esq., 376.
Wollaston Donation Fund, award of
the, to Dr. R. H. Traquair, Proc. 33.
Wollaston Medal, presentation of, to
Prof. P. Martin Dunean, Proc. 28.
Wyke quarry, vertical section of In-
ferior Oolite at, 589.
Yate rock, 78.
GENERAL INDEX.
Yeathouse, sandstone from, 12.
Yellowstone cafion, quartz rhyolite
from, 395.
district, vitreous tuff from the
Lower Geyser basin, 396; spheru-
litic rock from, 394; obsidian from,
391-594.
park, map of part of, 400.
Y Foel, section through, 159.
Ynyslas, 42.
Yonne, Upper Jurassic rocks of the,
valley, map of the, south of
Auxerre, 534.
Yoredale grit, from Shalk Beck, con-
stitution of 11; analysis of, 21.
END OF VOL, XXXVII.
Printed by TAYLOR and Francis, Red Lion Court; Fleet Street.
PROCEEDINGS
OF THE
GEOLOGICAL SOCIETY OF LONDON.
SESSION 1880-81.
November 3, 1880.
Rosert Erneriper, Esq., F.R.S., President, in the Chair.
Bernard Barham Woodward, Esq., 19 Stowe Road, Shepherd’s
Bush, W., was elected a Fellow of the Society.
The List of Donations to the Library was read.
The following specimens were presented to the Museum :—
Twenty specimens of Carboniferous Limestone Fossils from Flat-
head River, Rocky Mountains (49th Parallel N.W. America), pre-
sented by H. Bauerman, Esq., F.G.S.
The President announced that the original portrait of Dr. William
Smith, painted by M. Fourau in the year 1837, had been presented
to the Society by William Smith, Ksq., of Cheltenham.
The following communications were read :—
1. “On the Serpentine and Associated Rocks of Anglesey, with a
Note on theso-called Serpentine of Porthdinlleyn (Caernarvonshire).”’
By Prof. T. G. Bonney, M.A., F.R.S., Sec. G.S.
2. “ Note on the Occurrence of Remains of Recent Plants in
Brown Iron-ore.” By J. Arthur Phillips, Esq., F.G.S.
3. “ Notes on the Locality of some Fossils found in the Carboni-
ferous Rocks at T’ang Shan, situated, in a N.N.E. direction, about
120 miles from Tientsin, in the province of Chih Li, China.” By
VOL, XXXVII. a
2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
James W. Carrall, Esq., F,G.S. With a Note by Wm. Carruthers,
Esq., F.R.S., F.G.S.
The following specimens were exhibited :—
Rock-sections and specimens of rocks from Anglesey and Porth-
dinlleyn, exhibited by Prof. T. G. Bonney in illustration of his
aper.
y ate of recent plants in brown iron-ore, exhibited by J.
Arthur Phillips, Esq., in illustration of his paper.
Carboniferous plant-remains, from T’ang Shan, Chih Li, China,
exhibited by J. W. Carrall, Hsq., in illustration of his paper.
Sections of Devonian Corals, Agates, and Mocha Stones, exhibited
by S. H. Needham, Esq., to illustrate a new method of mounting
large sections of fossils, and minerals, and other natural-history
objects (such as Lepidoptera), so as to exhibit both the upper and
under surfaces at one view.
November 17, 1880.
Rosert ErHeripesr, Hsq., F.R.S., President, in the Chair.
Prof. Joseph Henry Tompson, of the Auckland College, Auckland,
New Zealand, was elected a Fellow of the Society. ‘
The names of the following Fellows in arrear to the Society were
read out by the President for the first time, in accordance with
Section VI. B, Article 6, of the Bye-laws:—W. H. Peacock, Esq.,
and W. Salmon, Hsq.
The List of Donations to the Library was read.
The Presipent called attention to the portrait of Dr. William
Smith, presented to the Society by his grand-nephew, Mr. W. Smith,
of Cheltenham, which was then suspended behind the chair, and
expressed his great satisfaction at this most interesting picture being
in the possession of the Society.
Mr. W. W. Smyrta expressed the satisfaction that all must feel
in possessing a genuine relic of this eminent stratigraphical geologist.
Now this one, which had been so liberally presented to the Society,
was a most indubitable portrait of the most conspicuous founder of
English geology. That portrait was painted by M. Fourauin 1837,
and was certainly an admirable likeness. The Society was deeply
indebted to the donor, Mr. W. Smith, the cousin of the late valued
Prof. Phillips. The portrait now hanging on the wall was engraved
in Prof. Phillips’s ‘ Life’ of his uncle. He proposed a hearty vote
of thanks to the donor.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 3
Mr. Evans rose with great pleasure to second the vote of thanks
proposed by Mr. Warington Smyth. The portrait was indeed
replete with interest, not only to English geologists but to all
geologists in the world. An additional interest attaching to the
portrait was that we had the whole history of it from Dr. Smith’s
own hand, an extract from which Mr. Evans read. The portrait
was an admirable one. He hoped that in the future Mr. Smith’s
example would be followed, and that we should see many other por-
traits of eminent geologists on the Society’s walls. The Society
was also deeply indebted to the President for the interest which he
had taken in the matter.
The vote of thanks was carried by acclamation.
The following communications were read :—
1. *¢ On abnormal Geological Deposits in the Bristol District.”
By Charles Moore, Esq., F'.G.S.
2. “ Interglacial Deposits of West Cumberland and North Lanca-
shire.” By J. D. Kendall, Esq., C.E., F.G.S.
Specimens from deposits in the Bristol District were exhibited by
Mr. Moore in illustration of his paper.
December 1, 1880.
Rosert Erueriper, Esq., F.R.S., President, in the Chair.
William Heward Bell, Esq., Hast Shefford House, Hungerford ;
William Jackson, Esq., Vernon Terrace Schools, Northampton ;
Peregrine Propert Lewes, Esq., M.A., L.L.M., 84 Kensington Gar-
dens Square, W.; William Libbey, Hsq., Jun., M.A., D.Sc., Princeton
College, Princeton, New Jersey, U.S.A.; David Morgan Llewellin,
Esq., Bryn Gomer, near Pontypool, Monmouthshire; John Mar-
shall, Esq., Sowerby Bridge, near Halifax; Cyril Parkinson, Esq.,
Rock Cottage, Ventnor, Isle of Wight, and Farnsfield, Southwell,
Notts; Cornelius McLeod Percy, Esq., The Grove, Standish, Wigan ;
Thomas John Robinson, Esqg., Melbourne Street, Longton, Stoke-
on-T'rent; Rey. Alfred Rose, M.A., Emmanuel College, Cambridge ;
Beeby Thompson, Esq., F.C.8., Abington Street, Northampton; and
Stuart Crawford Wardell, Esq., Doe Hill House, Alfreton, Derby-
shire, were elected Fellows of the Society.
The names of the following Fellows in arrear to the Society were
read out by the President for the second time, in aceordance with.
4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Section VI. B, Article 6, of the Bye-laws:—W. H. Peacock, Esq.,
and W. Salmon, Esq.
The List of Donations to the Library was read.
The following communications were read :—
1. “On Remains of a small Lizard from the Neocomian Rocks of
Comén, near Trieste, preserved in the Geological Museum of the
University of Vienna.” By Prof. H. G. Seeley, F.R.S., F.G.S.
2. “On the Beds at Headon Hill and Colwell Bay in the Isle of
Wight.” By H. Keeping, Esq., and HK. B. Tawney, Esq., M.A.,
F.G.S.
Specimens were exhibited by Prof. Seeley and Messrs. Tawney and
Keeping in illustration of their papers.
December 15, 1880.
Roser Erueriper, Esq., F.R.S., President, in the Chair.
William Elijah Benton, Esq., Assoc. R.S.M., Highfield House,.
Heather, near Ashby-de-la-Zouch ; Rev. George Clements, 26 St.
Martin’s Road, Stockwell; J. Kerr Gulland, Esq., C.E., 6 a Victoria
Street, S.W., and Ball’s Pond Road, N.; Francis T. 8. Houghton,
Ksq., B.A., Wynnstay, Balsall Heath, Birmingham ; George Bingley
Luke, Esq., Northbank House, Prestonpans, N.B.; and William
Mansell MacCulloch, Esq., MD., 12 Cork Street, Burlington Gardens,
W., were elected Fellows; and Professor Luigi Bellardi, of Turin,
and Dr. M. Neumayr, of Vienna, Foreign Correspondents of the
Society.
The List of Donations to the Library was read.
The following communications were read :—
1. “On the Constitution and History of Grits and Sandstones.”
By John Arthur Phillips, Esq., F.G.S.
The Chair was then taken by J. W. Hutxz, Esq., F.RS.,
V.P.G.S.
2. “ On a New Species of T'rrgonza from the Purbeck Beds of the
Vale of Wardour.” By R. Etheridge, Esq., F.R.S., President. With
a Note on the Stratigraphical position of the Fossil by the Rev. W.
R. Andrews.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 5
The following specimens were exhibited :—
Specimens exhibited by Messrs. J. Arthur Phillips and R. Ethe-
ridge in illustration of their papers.
Specimens of Crinoids from the Carboniferous Limestone, and a
pair of candlesticks turned out of Carboniferous Limestone, exhibited
by Prof. James Tennant, F.G.S.
January 5, 1881.
Rozert ErHeriner, Esq., F.R.S., President, in the Chair.
George C. Crick, Esq., 9 Gwyn Street, Bedford; and Arthur S$.
Reid, Esq., B.A., 12 Bridge Street, Canterbury, were elected Fellows
of the Society.
The List of Donations to the Library was read.
The following communications were read :—
1. “The Archean Geology of Anglesey.” By C. Callaway, Esq.,
M.A., D.Sc., F.G.S. With a Note on the Microscopic Structure of
some of the Rocks, by Prof. T. G. Bonney, M.A., F.R.S., Sec.G.5.
2. “The Limestone of Durness and Assynt.” By C. Callaway,
Esq., D.Sc., F.G.8.
3. “Ona Boulder of Hornblende-Picrite near Pen-y-Carnisiog,
Anglesey. By Prof. T. G. Bonney, M.A., F.R.S., Sec.G.8.
The following specimens were exhibited :—
Specimens of the results of some experiments in the formation
of Agates &c. exhibited by EH. A. Pankhurst, Esq., and James
TAnson, Esq., F.G.S.
Rock-specimens and microscopic sections exhibited by Dr. Calla-
way and Prof. Bonney, in illustration of their papers.
January 19, 1881.
Rosrrt Ernzriper, Esq., F.R.S., President in the Chair.
Jabez Church, Esq., M.Inst.C.E., 178 Great George Street, West-
minster, 8.W.; George Augustus Freeman, Esq., B.Sc. Lond., 6
VOL. XXXVII. b
6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Macduff Terrace, Danby Street, Peckham, 8.H.; Charles Horsley,
Ksq., C.H., 174 Highbury New Park, N.; Edwin Simpson-Baikie,
Ksq., F.L.S., United University Club, Pall Mall Hast, S.W.; and
Charles John Wood, Esq., M.Inst.C.E., 2 Selbourne Terrace, Bradford,
Yorkshire, were elected Fellows of the Society. .
The List of Donations to the Library was read.
The President called attention to the valuable donation made to
the Library by Dr. J. J. Bigsby, F.B.S., F.G.8., of the set of six
volumes of the ‘ Reports of the Geological Survey of Illinois,’ the
last four volumes of which are extremely rare on this side of the
Atlantic, 1f not almost unique. A special vote of thanks was passed
to Dr. Bigsby for his present.
The following communications were read :—
1. ‘Further Notes on the Family Diastuporide, Busk.” By G. R.
Vine, Esq. Communicated by Prof. P. Martin Duncan, M.B.Lond.,
PSs, EGS.
2. ‘Further Notes on the Carboniferous Fenestellide.” By G.
W. Shrubsole, Esq., F.G.S.
The following specimens were exhibited :—
Specimens of Opal, Chalcedony, &c., from Australia, exhibited by
Prof. James Tennant, F.G.S.
Specimens of Fenestellide, exhibited by Mr. Shrubsole in illus-
tration of his paper.
ie ce
February 2, 1881.
Roserr Ernertper, Ksq., F.R.S., President, in the Chair.
Joseph Groves, Esq., B.A., M.B. Lond., Carisbrooke, Isle of Wight ;
George Lewis, Esq., Green Hill, Derby; Rev. Edouard Méchin, 8.J.,
St. Beuno’s College, St. Asaph, North Wales ; James Osborne, Esq.,
Rio Tinto, Province of Huelva, Spain; and the Rey. William Shar-
inan, 20 Headland, Plymouth, were elected Fellows of the Society.
The List of Donations to the Library was read.
The following communications were read :—
1. “ On the Coralliferous Series of Sind, and its connexion with
the last Upheaval of the Himalayas.” By Prof. P. Martin Duncan,
M.B.Lond., F.R.8., F.G.S.
2. “On two new Crinoids from the Upper Chalk of Southern
Sweden.” By P. H. Carpenter, Esq., M.A. Communicated by
Prof. P. Martin Duncan, M.B.Lond., F.R.S., F.G:S.
PROCEEDINGS OF THE GEOLOGICAL SOCIDTY. 7
The following specimens were exhibited :—
A specimen of a new Crinoid, exhibited by Mr. Carpenter in
illustration of his paper.
Microscopic sections of Meteorites, exhibited by Dr. Otto Hahn,
of Reutlingen.
In explanation of the latter the following remarks were addressed
on behalf of Dr. Hahn to the President and Fellows present :—
“Dr. Hahn, in inviting you to examine the microscopical speci-
mens of meteorites which he has prepared, and in order to assist
you in determining the character of the forms and structures which
you will find exhibited in them, desires to present a short summary
of the negative considerations which forbid that such structures
should be classed among crystalline forms.
* As is well known, the chondrites, the species of meteorites
from which his specimens are prepared, consist, besides the metals
which they enclose, of the minerals enstatite and olivine.
“‘ Tn his work on the meteorites and their organisms, lately pub-
lished, Dr. Hahn has given photographs of 130 different forms and
structures. Now if these structures are crystalline, the two
minerals in question would present themselves in at least 130 dif-
ferent forms and structures, although the absence of all structure is
recognized as a fundamental principle of the theory of minerals.
“ Again, the structures exhibited by the chondrites cannot be
due to slaty cleavage, since olivine has no slaty cleavage, and that of
enstatite and of uther minerals does not appear under the micro-
scope, or else presents itself there under totally different forms.
“The greatest importance, however, is to be attached to the total
absence of all polarized light exhibited by the two minerals as oc-
curring in the meteorites. The contained forms and structures do
not polarize the light at all, or only very feebly, although the same
minerals, under ordinary circumstances, polarize light very strongly.
The absence of all aggregate polarization is especially noticeable, as
proving that these objects are not aggregates of crystals.
‘“¢ Should we still feel inclined to regard the enclosures as mineral
forms, and not as organisms, we must be struck by the utter absence
of all crystalline forms, especially in those very minerals which
always, and occasionally also in meteorites, appear in a crystallized
form.
“ Further, the external forms, and consequently the outlines of the
enclosures, harmonize so perfectly with their internal form and
structure, that we cannot entertain the idea that these enclosures
had been rolled about and ground down before they became finally
imbedded in the chondrites.
“The idea of an aggregate of crystals, if still looked upon with
favour, would be contradicted by the fact that the enclosed balls
or globes are all constructed excentrically, whereas all terrestrial
erystallites are formed concentrically.”
62
8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
ANNUAL GENERAL MEETING,
February 18, 1881.
Rozert Ernrriper, Esq., F.R.S., President, in the Chair.
REPORT OF THE CouNnciIL FoR 1880.
In presenting their Report for the year 1880, the Council of the
Geological Society have much gratification in announcing to the
Fellows that the affairs of the Society are in a much more satis-
factory position than at the dates of their last two Reports.
The number of new Fellows elected during the year is 60, of
whom 49 paid their fees before the end of the year, making, ah
14 previously elected Fellows who paid their fees in 1880, a total
accession during the year of 63 Fellows. Against this we have to
record the loss by death of 34 Fellows, and by resignation of only
9 Fellows, whilst 5 Fellows were removed from the list for non-
payment of Contributions, making a total loss of 48 Fellows. On
the year, therefore, we have an increase of 15 Fellows. But as of
the 34 Fellows deceased, 9 were compounders, and 9 con-contri-.
buting Fellows, the number of contributing Fellows is actually
increased by 25, being now 769.
The total number of Fellows and Foreign Members and Corre-
spondents was 1415 at the end of the year 1879, and 1432 at the
end of the year 1880.
During the year 1880 intelligence was received of the death of
1 Foreign Member and of 2 Foreign Correspondents. As two
vacancies existed in the list of Foreign Members at the end of the
year 1879, three Foreign Members were elected in 1880; and the
vacancies caused by these elections and by death in the list of
Foreign Correspondents, were all filled up during the year.
The total Receipts for the year 1880 were £2706 1s. 7d., being
£130 15s. 7d. more than the estimated Income for the year. The
total Expenditure, on the other hand, was £2520 18s. 9d., or
£154 4s. 1d. less than the estimate for the year. The actual excess
of Income over Expenditure was thus £185 2s. 10d.; and of this
amount a sum of £98 10s. was invested in the purchase of £100
Consols.
The Council have to announce the completion of Vol. XXXVI. of
the Quarterly Journal and the commencement of Vol. XX XVII.
The Council have further to announce the completion of the
a a a
ANNUAL REPORT. 9
printing of the Catalogue of the Library, which is now ready for
distribution to subscribers. It forms a volume of over 620 pages, or
about 100 pages more than was originally estimated ; but the Council
have not thought it desirable to increase the price of the volume.
It will accordingly be furnished to the Fellows at the price of five
shillings.
The Council have much pleasure in announcing that William
Smith, Esq., of Cheltenham, the grandnephew of Dr. ‘William Smith,
and cousin of the late Professor Phillips, has most liberally presented
to the Society the portrait of Dr. Smith which was formerly in Prof.
Phillips’s possession, and from which was engraved the small portrait
illustrating his ‘Memoir of William Smith.’ This picture, which is
admirable in itself, is of special interest to the Fellows of the
Geological Society, not only as an excellent portrait of one of the
great founders of their Science, but also from its historical associa-
tions, as its origin and mode of production have been described in
Dr. Smith’s own words in the ‘ Memoir’ just mentioned, as it bears
his handwriting on its back, and as it is the original of the engraved
portrait. For the due preservation of this valuable picture the
Council have ordered it to be suitably framed and covered with plate
glass, and to be suspended in a place of honour in the Meeting-room
of the Society. They hope that it may not long remain there in
solitude. In the mean-time four of the marble busts in the possession
of the Society (those, namely, of Greenough, Sedgwick, Murchison,
and Macculloch) have been arranged upon pedestals at the end of the
Meeting-room, where they may serve to cherish the memory of some
of those who have contributed the most to advance the Science of
Geology.
The Council have awarded the Wollaston Medal to Professor P.
Martin Duncan, F.R.S., F.G.8., in testimony of their high apprecia-
tion of his numerous and valuable paleontological memoirs, especially
on the Fossil Corals, as well as of his contributions to physical and
stratigraphical Geology.
The Murchison Medal, with the sum of Ten Guineas from the
proceeds of the Fund, has been awarded to Professor Archibald
Geikie, F.R.S., F.G.S., in recognition of his valuable contributions to
physical and stratigraphical Geology, particularly in relation to the
Old Red Sandstone of Scotland, and the Voleanic Geology of the
vicinity of Edinburgh and the Firth of Forth.
The Lyell Medal, with a sum of Twenty-five Pounds from the
proceeds of the Fund, has been awarded to Principal Dawson,
F.R.S., F.G.S., in recognition of his important contributions to the
Geology of Canada, and more especially of his investigations into the
Fossil Flora of the Devonian and Carboniferous Periods in America.
The Bigsby Medal has been awarded to Dr. Charles Barrois, of
Lille, as a testimony to the importance of his contributions to strati-
sraphical Geology, particularly with relation to the Cretaceous
system.
"The balance of the proceeds of the Wollaston Donation Fund
has been awarded to Dr. Ramsay H. Traquair, F.G.S., in recogni-
igo) PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
tion of the value of his researches upon the paleontology of Fossil
Fishes, and to aid him in pursuing his investigations.
The balance of the proceeds of the Murchison Donation Fund
has been awarded to Frank Rutley, Esq., F.G.8., as a token of
appreciation of his valuable memoirs on various petrological sub-
jects, and to assist him in carrying on his researches.
The balance of the proceeds of the Lyell Donation Fund has
been awarded in equal parts to G. R. Vine, Esq., in recognition of
the work done by him on the Carboniferous Polyzoa, and to assist
him in continuing his investigations ; and to Dr. Anton Fritsch, of
Prague, as a mark of the estimation in which his valuable contri-
butions to Palzontology are held, and to aid him in the production
of his important memoirs.
During the last Session, a subscription was set on foot among the
Fellows of the Society, which enabled the Assistant Secretary to
purchase four small plain Microscopes, for use, when required, at
the Evening Meetings of the Society. As the procuring the means
of illumination for the microscopes was attended with considerable
inconvenience and expense, the Council have decided to expend a
small portion of the proceeds of the Barlow-Jameson Fund in the
purchase of four of How’s Microscope Lamps.
REPORT OF THE LIBRARY AND Museum Committee,
Lnbrary.
Since the last Anniversary Meeting a great number of valuable |
additions have been made to the Library, both by donation and by
purchase. é
As Donations the Library has received 105 volumes of separately
published works and Survey Reports, and about 220 Pamphlets and
separate impressions of Memoirs; also about 102 volumes and 205
detached parts of the publications of various Societies, and 14
volumes of independent Periodicals presented chiefly by their re-
spective Lditors, besides 11 volumes of Newspapers of various
kinds. This will constitute a total addition to the Society’s Library,
by donation, of about 272 volumes and 220 pamphlets.
A considerable number of Maps, Plans, and Sections have been
added to the Society’s collections by presentation from various Geo-
logical Surveys, from the Ordnance Survey of Great Britain, and from
the French Depot de la Marine. Several Geological Maps of parti-
cular districts have also been presented by the authors. They
amount altogether to 348 sheets, and among them may be noted, as
especially valuable to the Society, 131 sheets of the Map of the
Geological Survey of Great Britain and Ireland.
The Books and Maps just referred to have been received from
ANNUAL REPORT, Mt
128 personal Donors, the Editors or Publishers of 15 Periodicals,
and 131 Societies, Surveys, or other Public Bodies, making in all
274 Donors,
By Purchase, on the recommendation of the Standing Library
Committee, the Library has received the addition of 46 volumes of
Books, and of 53 parts (making about 10 volumes) of Periodicals,
besides 12 parts of works published serially, the earlier portions of
which were obtained in previous years. Five Sheets of the Geolo-
gical Survey Map of France, and 4 sheets of a Map of the Bohe-
mian Coalfield, by Dr. Wolff, have been obtained by purchase.
The cost of Books and Periodicals during the year 1880 was
£73 2s. 3d., and of Binding £76 10s. 1d. The total expenditure
on account of the Library was thus £149 12s, 4d.
The Books in the Society’s Library are generally in good con-
dition; and a considerable number of old serial and other works,
of which the binding had been damaged by long use, have been
rebound or repaired. The Library continues to be much used by
the Fellows of the Society. :
Museum.
The Collections in the Museum remain in much the same con-
dition as at the date of the last Report of the Committee, the
Foreign Collections being all available for reference. The Egerton
Collection of Arctic Fossil Shells has been named and arranged by
Dr. J. Gwyn Jeffreys.
The following Donatisns have been made fo the Museum during
the year 1880 ;—A specimen of rock from the top of the Asnai
Heights, Cabul, presented by Lieut. F. Spratt, R.K., and 20 speci-
mens of Carboniferous-limestone Fossils from Flathead River, Rocky
Mountains, presented by H. Bauerman, Iisq., ¥.G.5.
12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
CoMPARATIVE STATEMENT OF THE NUMBER OF THE SOCIETY AT THE
CLOSE OF THE YEARS 1879 anp 1880. -
Dee. 31, 1879. Dec. 31, 1880.
Compoundersyee es ae DOs eee: 312
Contributing Fellows... .. TA” ibe ae. 769
Non-contributing Fellows . . 21s POON E 268
1334 1349
Honorary Members ...... Siny de en ee 3
Foreign Members ........ BOs he Mien 40
Foreign Correspondents... . AO seis cody te tone tie 40
1415 1432
General Statement explanatory of the Alterations in the Number of
Fellows, Honorary Members, &c. at the close of the years 1879 and
1880.
Number of Compounders, Contributing and Non- 1384
contributing Fellows, December 31, 1879.... }
Add Fellows elected during former year and paid
: 14
in 1880
Add Fellows elected and paid in 1880 ....... : 49
@:er7\0) ‘©) (a (e (e) © “0. ce) 1@ @ © (ee ie » © [ele « « (0 (e¢ je « 0) wy lene
1397
Deduct Compounders deceased ..............
Contributing Fellows deceased ........
Non-contributing Fellows deceased ....
Contributing Fellows resigned
Contributing Fellows removed
eecee ee eee
lacoae
1349
Members, and Foreign Correspondents,
December 31, 1879
Deduct Foreign Member deceased .. ..... 1
Foreign Correspondents deceased .. 2
Foreign Correspondents ee |
Number of Honorary Members, nets
Foreign Members
~I
Add Foreign Members elected .......... 3
Foreign Correspondents elected
|
|
ANNUAL REPORT.
Decrasep Frtiows.
Compounders (9).
Lord Belper. ) W. Gillespie, Esq.
T. Bell, Esq. | W. H. Holloway, Esq.
Col. W. G. Boyle. | EK. Walton, Esq.
Sir R. Burdett. S. V. Wood, Esq.
W. W. Collins, Esq.
Resident and other Contributing Fellows (16).
Prot. D. T. Ansted. D. Llewellin, Esq.
T. D. Bott, Esq. _ iH. Ludlam, Esq.
Lieut.-Gen. W. EK. D. Broughton. | Dr. E. Merypn.
E. W. Cooke, Esq. E. J. Smith, Esq.
J. Cope, Esq. T. Parry, Esq.
J. G. H. Godfrey, Esq. W. W. Stoddart, Esq.
J. Hamilton, Esq. : Rev. J. Clifton Ward.
W. G. Kell, Esq. E. B. Webb, Esq.
Non-contributing Fellows (9).
C. L. Bradley, Esq. | J. R. Logan, Esq.
R. Davey, Esq. Rey. 8. Lucas.
T. C. Eyton, Esq. | Prof. W. H. Miller.
W. Gray, Esq. | Dr. Jones Quain.
Very Rey. H. P. Hamilton.
Foreign Member.
Profyb ws Niyst
Foreign Correspondents.
Prof. W. P. Schimper. | M. J, A. H. Bosquet.
Fellows Resigned (9).
Rey. W. H. Allen. _ Lieut.-Col. C. Manby.
F. Campion, Esq. _ Lieut.-Col. E. B. Sladen.
S. N. Carvalho, Esq., Jun. _ H. B. Whitehead, Esq.
E. C. H. Day, Esq. | Capt. H. T, Wing.
H, Fox, Esq.
14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Fellows Removed (5).
Jonathan Harrison, Esq. W. Harrison Peacock, Esq.
J. Trubshaw Johnson, Esq. William Salmon, Esq.
Lewis Thomas Lewis, Esq.
The following Personages were elected from the List of Foreign Cor-
respondents to fill the vacancies in the List of Foreign Members
during the year 1889.
Professor Gustave Dewalque of Liége.
Professor Adolf Eric Nordenskiold of Stockholm.
Professor Ferdinand Zirkel of Leipzig.
The following Personages were elected Foreign Correspondents during
the year 1880,
Dr. Ferdinand von Hochstetter of Vienna.
Professor Leo Lesquereux of Columbus.
M. Alphonse Renard of Brussels.
After the Reports had been read, it was resolved :—
That they be received and entered on the Minutes of the Meeting,
and that such parts of them as the Council shall think fit be printed
and distributed among the Fellows,
It was afterwards resolvea :—
That the thanks of the Society be given to Sir P. de M. Grey-
Egerton, Bart., and Prof. A. C. Ramsay, retiring from the office of
Vice-President. ,
That the thanks of the Society be given to Dr. H. Hicks, Prof.
T. M‘Kenny Hughes, Prof. T. Rupert Jones, Prof. J. Prestwich, and
Prof. A. C. Ramsay, retiring from the Council.
After the Balloting-glasses had been duly closed, and the lists
examined by the Scrutineers, the following gentlemen were declared
to have been duly elected as the Officers and Council for the ensuing
year :—
ANNUAL REPORT, 15
OFFICERS,
PRESIDENT.
R. Etheridge, Esq., F.R.S.
VICE-PRESIDENTS.
J. Evans, D.C.L., LL.D., F.B.S.
J. W. Hulke, Esq., F.R.S.
Prof. J. Morris, M.A.
Tals Ob sont oni, dllb Dy Ine iigse
SHCRETARIES.
Prof. T. G. Bonney, M.A., F.R.S,
rote Wierd udde aks.
4
FOREIGN SECRETARY.
W. W. Smyth, Esq., M.A., F,R.S.
TREASURER.
J. Gwyn Jeffreys, LL.D., F.R.S.
COUNCIL.
H. Bauerman, Esq. W. H. Hudleston, Esq., M.A.
Rev. J. F. Blake, M.A. J. W. Hulke, Esq., F.R.S.
Prof. T. G. Bonney, M.A., F.R.S. |J. Gwyn Jeffreys, LL.D., F.R.S.
W. Carruthers, Esq., F.R.S. Prof. J. W. Judd, F.R.S.
Prof. P. M. Dune
an, M.B.,F.R.S. | Prof. N. 8. Maskelyne, M.P.,
Sir P. de M. Grey-Kgerton, Bart., M.A., F.R.S.
M.P., F.RS.
Prof. Morris, M.A.
R. Etheridge, Esq., F.R.S. J. A. Phillips, Esq.
J. Evans, D.C.L., LL.D., F.R.S. | F. W. Rudler, Esq.
Lieut.-Colonel H. H. Godwin- | Prof. H. G. Seeley, F.R.8.
Austen, F.R.S.
J. C. Hawkshaw,
W. W. Smyth, Esq., M.A., F.R.S,
Esq., M.A. H. C. Sorby, LL.D., F.R.S.
Rey. Edwin Hill, M.A, ; |H. Woodward, LL.D., F.R.S,
16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
LIST OF
THE FOREIGN MEMBERS
OF THE GEOLOGICAL SOCIETY OF LONDON, tn 1880.
Date of
Election.
1827. Dr. H. von Dechen, Bonn.
1829. Dr. Ami Boué, Vienna.
1844, William Burton Rogers, Esq., Boston, U. S.
1848. James Hall, Esq., Albany, State of New York.
1850. Professor Bernhard Studer, Berne.
1851. Professor James D. Dana, New Haven, Connecticut.
1853. Count Alexander von Keyserling, Raykiill, Russia.
1855. Professor L.G. de Koninck, ee
1854. M. Joachim Barrande, Prague.
1856. Professor Robert Bunsen, For. Mem. R.S., Heidelberg.
1857. Professor H. R. Goeppert, Breslau.
1857. Professor H. B, Geinitz, Dresden.
1857. Dy. Hermann Abich, Vienna.
1859. Professor A. Delesse, Paris.
1859. Dr. Ferdinand Roemer, Bresiav.
1860. Dr. H. Milne-Edwards, For. Mem. R.S., Paris.
1862. Professor Pierre Merian, Basle.
1864. M. Jules Desnoyers, Paris.
1866. Dr. Joseph Leidy, Philadelphia.
1867. Professor A. Daubrée, Paris.
1870. Professor Oswald Heer, Zurich.
1871. Dr. 8. Nilsson, Lund.
1871. Dr. Henri Nyst, Brussels. (Deceased. )
1871. Dy. Franz Ritter von Hauer, Vienna.
1874. Professor Alphonse Favre, Geneva.
1874. Professor E. Hébert, Paris.
1874. Professor Edouard Desor, Neuchdtel.
1874. Professor Albert Gaudry, Paris.
1875. Professor Fridolin Sandberger, Wiirzburg.
1875. Professor Theodor Kjerulf, Christianta.
1875. Professor F. August Quenstedt, Tiibingen.
1876. Professor E. Beyrich, Berlin.
1877. Dr. Carl Wilhelm Giimbel, Munich.
1877. Dr. Eduard Suess, Vienna.
1879, Dr. F. V. Hayden, Washington.
1879. Major-General N. von Kokscharow, St. Petersburg.
1879. M. Jules Marcou, Salus.
1879. Dr. J. J. S. Steenstrup, For. Mem. R.8., Copenhagen.
1880. Professor Gustave Dewalque, Liége.
1880. Professor Adolf Eric Nordenskidld, Stockholm.
1880. Professor Ferdinand Zirkel, Lezpzzg.
ANNUAL REPORT.
LIST OF
THE FOREIGN CORRESPONDENTS
OF THE GEOLOGICAL SOCIETY OF LONDON, ry 1880.
Date of
Election.
1863. Dr. G. F. Jager, Stuttgart.
1863. M.S. Lovén, Stockholm.
1863. Count A. G. Marschall, Vrenna.
1863. Professor G. Meneghini, Pisa.
1863. Signor Giuseppe Ponzi, Rome.
1865. Signor Quintino Sella, Rome.
1865. Dr. F. Senft, Evsenach.
1864. M. J. Bosquet, Maestricht. (Deceased.)
1864. Dr. Charles Martins, Montpellier.
1866. Professor J. P. Lesley, Philadelphia.
1866. Professor Victor Raulin, Bordeaux.
1866. Baron Achille de Zigno, Padua.
1870. Professor Joseph Szabd, Pesth.
1870, Professor Otto Torell, Lund.
1871. M. Henri Coquand, Marseilles.
1871. Professor Giovanni Capellini, Bologna.
1872. Herr Dionys Stur, Vienna.
1872. Professor J. D. Whitney, Cambridge, U. S.
1874, Professor Igino Cocchi, Florence.
1874. M. Gustave H. Cotteau, Aaverre.
1874. Professor W. P. Schimper, Strasburg. (Deceased.
1874. Professor G. Seguenza, Messina.
1874. Dr. J. S. Newberry, New York.
1874. Dr. T. C. Winkler, Haarlem.
1875. Professor Gustav Tschermak, Vienna.
1876. Professor Jules Gosselet, Lille.
1876. Professor Ludwig Riitimeyer, Basle.
1877. Professor George J. Brush, New Haven.
1877. Professor A. L. O. Des Cloizeaux, For. Mem.R.S., Paris.
1877. Professor KE. Renevier, Lausanne.
1877. Count Gaston de Saporta, Adx-en-Provence.
1879. Professor Pierre J. van Beneden, For.Mem.R.8., Louvain.
1879. M. Edouard Dupont, Brussels.
1879. Professor Guglielmo Guiscardi, Naples.
1879. Professor Franz Ritter von Kobell, Munich.
1879. Professor Gerhard vom Rath, Bonn.
1879. Dr. Emile Sauvage, Paris.
1880. Dr. Ferdinand von Hochstetter, Vienna.
1880. Professor Leo Lesquereux, Columbus.
1880, M. Alphonse Renard, Brussels.
18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
AWARDS OF THE WOLLASTON MEDAL
UNDER THE CONDITIONS OF THE ‘‘ DONATION FUND”
ESTABLISHED BY
WILLIAM HYDE WOLLASTON, M_D., F-.BS., F.G.S., &e.
“To promote researches concerning the mineral structure of the earth,
and to enable the Council of the Geological Society to reward those
individuals of any country by whom such researches may hereafter be
made,”—“ such individual not being a Member of the Council.”
1831. Mr. William Smith. 1959, | Herr Hermann von Meyer.
1835. Dr. G. A. Mantell. ' (Mr. James Hall.
1836. M. L. Agassiz. 1859. Mr. Charles Darwin.
1837, ae T. P. Cautley. 1860. Mr. Searles V. Wood.
Dr. H. Falconer. 1861. Professor Dr. H. G. Bronn.
1838. Professor R. Owen. 1862. Mr. R. A. C. Godwin-
1839. Professor C. G. Ehrenberg. Austen.
1840. Professor A. H. Dumont. 1863. Professor Gustav Bischof.
1841. M. Adolphe T. Brongniart. 1864. Sir R. I. Murchison.
1842. Baron L. von Buch. 1865. Mr. Thomas Davidson.
1843. {M. Elie de Beaumont. 1866. Sir Charles Lyell.
\M.P. A. Dufrénoy. 1867. Mr. G. Poulett Scrope.
1844. The Rev. W. D. Conybeare. | 1868. Professor Carl F. Naumann.
1845. Professor John Phillips. 1869. Dr. H. C. Sorby.
1846. Mr. William Lonsdale. 1870. Professor G. P. Deshayes.
1847. Dr. Ami Boué. 1871. Professor A. C. Ramsay.
1848. The Rey. Dr. W. Buckland. | 1872. Professor J. D. Dana.
1849. Professor Joseph Prestwich. | 1873. Sir P. de M. Grey-Kgerton.
1850. Mr. William Hopkins. 1874, Professor Oswald Heer.
1851. The Rev. Prof. A. Sedgwick. | 1875. Professor L. G. de Koninck.
1852. Dr. W. H. Fitton. 1876. Professor T. H. Huxley.
1853. M. le Vicomte A. d’Archiac. | 1877. Mr. Robert Mallet.
M. E. de Verneuil. 1878. Dr. Thomas Wright.
1854. Sir Richard Griffith. 1879. Professor Bernhard Studer.
1855. Sir H. T. De la Beche. 1880. Professor Auguste Daubrée.
1856. Sir W. HE. Logan. 1881. Professor P. Martin Duncan.
1857. M. Joachim Barrande. re
ANNUAL REPORT.
AWARDS
OF THE
Ng
BALANCE OF THE PROCEEDS OF THE WOLLASTON
“ DONATION-FUND.”
1831.
18383.
1854.
18368.
1836.
1838.
1839.
1840.
1841.
1842.
1848.
1844.
1845.
1846.
1847.
1848.
1849.
1850.
1851.
1852.
1853.
1854,
1855.
1856.
1857.
Mr. William Smith.
Mr. William Lonsdale.
M. Louis Agassiz.
Dr. G. A. Mantell.
Professor G. P. Deshayes.
Professor Richard Owen.
Professor G. C. Ehrenberg.
Mr, J. De Carle Sowerby.
Professor Edward Forbes.
Professor John Morris.
Professor John Morris.
Mr. William Lonsdale.
Mr. Geddes Bain.
Mr. William Lonsdale.
M. Alcide d’Orbigny.
} Cape-of-Good-Hope Fossils.
M. Alcide d’Orbigny.
Mr. William Lonsdale.
Professor John Morris.
M. Joachim Barrande.
Professor John Morris.
Mr. 8. P. Woodward.
Drs. G. and F’. Sandberger.
Professor G. P, Deshayes.
Mr. 8S. P. Woodward.
| 1868.
1859.
1860.
1861.
| 1862.
_ 1868.
| 1864.
— 1865.
1866.
| dushovi,
| 1868.
| 1869.
1870.
1871.
S72:
| 1878.
— :1874.
| 1875.
elisiG:
| Men
1878.
| 1879.
1880,
1881.
Professor L. G. de Koninck. |
|
Mr. James Hall.
Mr. Charles Peach.
Professor T. Rupert Jones.
sae W. K. Parker.
Professor A. Daubrée.
Professor Oswald Heer.
Professor Ferdinand Senft.
Professor G. P. Deshayes.
Mr. J. W. Salter.
Dr. Henry Woodward.
Mr. W. H. Baily.
M. J. Bosquet.
Mr. W. Carruthers.
M. Marie Rouault.
Mr. R. Etheridge.
Mr. James Croll.
Professor J. W. Judd.
Dr. Henri Nyst.
Mr. L. C. Miall.
Professor Giuseppe Seguenza.
Mr. R. Etheridge, Jun.
Mr. W. J. Sollas.
Mr. 8. Allport.
Mr. Thomas Davies.
Dr. R. H. Traquair.
AWARDS OF THE MURCHISON MEDAL
AND OCF THE
ROCEEDS OF “THE MURCHISON GEOLOGICAL FUND,”
ESTABLISHED UNDER THE WILL OF THE LATE
SIR RODERICK IMPEY MURCHISON, Banr., F.R.S., F.GS.
“To be applied in every consecutive year in such manner as the Council
of the Society may deem most useful in advancing geological science,
20
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
whether by granting sums of money to travellers in pursuit of know-
ledge, to authors of memoirs, or to persons actually employed in any
inquiries bearing upon the science of geology, or in rewarding any
such travellers, authors, or other persons, and the Medal to be given
to some person to whom such Council shall grant any sum of money
or recompense in respect of geological science.”
1873. My. William Davies. Medal. | 1877. Rev. W. B. Clarke. Medal.
1873. Professor Oswald Heer. 1877. Rev. J. F. Blake.
1874. Dr. J. J. Bigsby. Medal. 1878. Dr. H. B. Geinitz. Medal.
1874. My. Alfred Bell. 1878. My. C. Lapworth.
1874. Mr. Ralph Tate. 1879. Professor F. M‘Coy. Medal.
1875. Mr. W. J. Henwood. Medal. | 1879. My. J. W. Kirkby.
1875. Prof. H. G. Seeley. 1880. Mr. R. Etheridge. Medal.
1876. Mr. A.R.C. Selwyn. Medal. | 1881. Professor A.Geikie. Medal.
1876. Mr. James Croll. 1881. Mr. F. Rutley.
AWARDS OF THE LYELL MEDAL
AND OF THE
PROCEEDS OF THE “LYELL GEOLOGICAL FUND,”
ESTABLISHED UNDER THE WILL AND CODICIL OF THE LATE
SIR CHARLES LYELL, Barrt., F.RS., F.G.S.
The Medal ‘‘to be given annually” (or from time to time) “as a mark of
honorary distinction as an expression on the part of the governing
body of the Society that the Medallist has deserved well of the
Science,” —‘‘not less than one third of the annual interest [of the
fund] to accompany the Medal, the remaining interest to be given in
one or more portions at the discretion of the Council for the encou-
ragement of Geology or of any of the allied sciences by which they
shall consider Geology to have been most materially advanced.”
1876. Professor John Morris. | 1879. Professor H. A. Nicholson.
Medal. 1879. Dr. Henry Woodward.
1877. Dr. James Hector. Medal. 1880. Mr. John Evans. Medal.
1877. Mr. W. Pengelly. 1880. Professor F. Quenstedt.
1878. Mr. G. Busk. Medal. 188]. Professor J. W. Dawson.
1878. Dr. W. Waagen. Medal.
1879. Professor Edmond Hébert. | 1881. Dr. Anton Fritsch.
Medal. 1881. Mr. G. R. Vine.
nt
ANNUAL REPORT. 21
AWARDS OF THE BIGSBY MEDAL,
FOUNDED BY
Dee I biG SBN B.S. E. Gas:
To be awarded biennially “as an acknowledgment of eminent services
in any department of Geology, irrespective of the receiver’s country ;
but he must not be older than 45 years at his last birthday, thus
probably not too old for further work, and not too young to have done
much.”
1877. Professor O. C. Marsh. 1881. Dr, Charles Barrois.
1879. Professor E. D, Cope.
VOL. XXXVII. C
22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Estimates for
INCOME EXPECTED.
Ls. 8... Sane
Due for Subscriptions for Quarterly Journal... 3 5 4
Due for Arrears of Annual Contributions ...... AO) ©
Due for Arrears of Admission-fees ........... 5 4 Do
257 7 4
Estimated Ordinary Income for 1881 :—
Annual Contributions from Resident Fellows, and Non-
residentsiof lSo9 tonlSGla ee seen 1400 0 O
Admission=fees.. oii. csin «Us wise candela 252 0 0
Compositions... a! als fuk Jo8s Srenaa2 eabene nancies een 241 10 0
Annual Contributions invadvancer). 25h e eee 1212 0
Dividends on Consols and Reduced 3 per Cents .......... 238 10 2
Advertisements in Quarterly Journal..............0..... 7 10°70
Sale of Transactions, Library-catalogues, Orme-
rod’s Index, and Hochstetter’s New Zealand... 30 0 0
Sale of Quarterly Journal, including Longman’s
DECOUNE| 25.52 Cinnge a te a milecn cpa ace teialleuor ata keno 215 0 0
Sale of Geological Map, including Stanford’s
QCCOUNEM Ht ier crete laytelo i ciicoe 1 orice emer 25 0 0
— 270 0 0
sale of Stock for Library Catalogue) 73.5. i100 eee 268 10 0
£2947 19 6
J.GWY¥N JEFFREYS, Treas.
14 Hiding Were
FINANCIAL REPORT, 23
the Year 1881.
EXPENDITURE ESTIMATED.
House Expenditure:
eRe sand ENSUTANCOT cans ssececisd-ssewscascedes es 33 10 O
ROE oe on Rea ea ene vce angels ctesaredoedieiesiae 25 0 0
ie rae oer tonics de datciousaiona ce otanetweuins 40 0 0
PISSED GLEE OR cr ee a )oloe cise saldniiclesiice eclecaenioees 740) Wa)
House-repairs and Maintenance.................. 35 0 0
PeeMeROE MCLE AMMAG oan cssjosrascvseecactesedeocisae 2070) 0
Washing and sundry small Expenses ......... 40 0 0
12D 2) MIGHT) LaseAndansossenocopseagenoLosuacoocs 20 OF 50
233 10 0
Salaries and Wages:
BS AAMT ESCCECLATY) Gi si\-sessiccsensssceesvceseowieas 350 0 0
re ee anes cect enue cacste denies Sawsesacte’s 140 0 0
Assistant in Library and Museum ............... MOTO 0
VOR SLOW ATO: iio. cece segeect eevee abeeastedeaces 105 0 0
1S UO UISCUTE TG Ue RSA Ae Rae ee ee ee 40 0 O
Ere el Ls Oper coe acta: cae cratic le sve sins aaisroaleSie oe 32 10 O
Charwoman and Occasional Assistance......... 50 0 0
Attendants at Meetings ...............000+Rsceoee 810 0
PMCCOMM ATU Seresetinit nace sna nsicisesecweasinsadscseetee tS) a)
Official Expenditure :
SIDE OIILGIAY oe SRB eEE ROAR Ene cere eee rier 2a nO @
Miscellaneous Printing ..0.s.cle.sceessceees ccna 2a 0) 10
Diaeramistat Meetings .....2.....ss-0-0reeeeeeeneins DO 50
Postages and other expenses ............ceeeeees com OwEO
129) 05-0
LL ETE 900060 6 UR COCO IOC Cer nienCI Cn ia TEz aren ir ne sa NE 150 0 0
Aine PTIMPMEM ASE Seo Foye 5 oo o\iuo, 6-5 514 4 oie, sore = ald. olezeye olinye! aye SG
Publications:
SeeOO A CAIMMIA NS. cance oebab see ineis cetenascnaisniesine uses 50 0 0
@uarterly Journal ../..........:- £915 0 O
a - Commission,
Postage, and Addressing... 85 0 0
—- -1000 0 0
si eOMBCMOWSS.- oon. -ceceesscssecnseevevagesmsessens 36 0 0
Abstracts, including Postage ............0+.c000 95 0 O
Wibtanyp Catalogue. ..2..-.n2.cececeecesoasnsennci 268 10 0
1449 10 0
Balance in favour of the Society........ ene LOO leas
£2947 19 6
Ne ne nl
24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Income and Expenditure during the
RECEIPTS. i
eg ds Eset
Balance in Bankers’ hands, 1 January 1880. 14 4 1
Balance in Clerk’s hands, 1 January 1880. 111 8
— 15 15 9
Compositions aces: « . Someta menor we ranratieiete easton 241 10 OU
Arrears of Admission-fees.............. 88 4 0
Admuissiom=tceslSS On) coch-pae une etait 308 14 0
a 396 18 0
Arrearaor Annual Contrlbubionsi nen ceeia ele 189 11 6
Annual Contributions for 1880, viz. :—
Resident Fellows ......... £1329 16 6
Non-Resident Fellows ... 26 15 6
——_—_— 1356 12 0
Annual Contributions in advance...... Bebe ObSoSccK RS Ney (G)
Journal Subscriptions mm advancela-....- era ieee 016 4
Dividends ony Consols) 5 ee 20fa= MeO
. Reduced 3 per Cents. ...... 30 Sine
ee
Taylor & Francis: Advertisements in Journal, Vol.35.. 717 O
Publications :
Salevordournaly Violsal=3nmice eee eeeces 126 13 8
Ms VOLTS Rees aan neers SB) yy ak
SalevorMl:ansachions ence eee OMA 9
Salevon lnbrany Catalogel cuss. scascscecesoes my 0
Salevol Geological: Menpiienecncenescaacseaee 26 0 10
SalevormOnrmerod’slindexis. 0 aera 2 210
Sale of Hochstetter’s New Zealand ......... 016 O
*Due from Messrs. Longman, in addition to the
above, on sournals Viola 30) sce sue ee seen eee 6b Seat
tDue from Stanford on account of Geological Map SelOel
£69) 1392
LM 17 4
We have compared the Books and
Accounts presented to us with this
statement, and we find them to agree.
(Signed) J. CLARKE HAWKSHAW,
F, G. HILTON PRICE, \ Auditors.
27 Jan. 1881.
FINANCIAL REPORT. 25
Year ending 31 December, 1880.
EXPENDITURE.
General Expenditure: CSA / Ly) Ges de
SCR ete sre t ate isceme en eebwhiayineaatvor is ousiedes So LO
MBE UMSUPATICO I ye crs.e cc worsens seis scienwohie eer 12050
PE UISK nd GUN Clee Reels ict cn ncnctee ese a rancedease acces 20 15 6
EVOQUSE-FEMAITA Ns (een ciathialeces aceiee santa ee teeioc ve sees 33 16 8
BETO ee ee ncaa cei etic te cocci asvacees oanhcs 388 15 O
Ti EING, cae SSeS stein BAO CeCE ae eR ice eee ene By IIA
Miscellaneous House-expenses.........0..ceee0s 7,
SITILOTIGIAY | dbangetBoroakaeeueee Cho bdsnee nebecenper nce 20 10 4
Miscellaneous Printing. cecc cs.) -cedescscesensne 2, dG
Menta Meetim SS. .c..5- 0 cistvaviace ese sce Hapieusiorane US IG)
—— go2 924
Salaries and Wages :
Assistant Secretary (five quarters) ............ 437 10 O
CLSTES axed pe RS HOSE IRSA I ae ge nates eee 140 0 0
Library and Museum Assistants ............... 140 8 4
MIMO LSC MSEC WAL) nieces ececoniseaerisentiscese siecle 105 0 O
MOUSE MIEA IG tye. ccs Sogo eso eee cc caide e's pees 40 0 0
Wecasional Attendants: oi. so. ce .edesrccensercnaee 8 10 O
BARC UMELETILS) wanes casey ie oetacls snus cincas access COMER
——— 878 15 4
LLIN? oe ne eee SOR eee 149 12 4
Miscellaneous Expenses, including postages ........ Wl ie
Wiierans at Meevings 22.25. 6 sc ieee ec bee ees 314 0
exesamentsim 6100 Consol, . 2 ..0..0e0c2 sere ee 98 10 0
Publications :
reolOmed le Map rrcesccarscctssssossescanoss cca: Ih igs ©
OMEN aeVOlS lO) is agendas case tele eases eee 7
3 Wo lithon ttaeca cece ashes £877 10 5
Commission,
Postage, and Addressing... 82 15 11
6 4
PMS ACU NH saat nal taete sna ts ing slala oc urisenitiacoasise 95) on okt
—— 106418 0
Balance in Bankers’ hands, 31 Dec. 1880.. 96 0 6
Balance in Clerk’s hands, 31 Dec. 1880 .. 6 8 1
——__—_ 1092 8 7
AEA OM Lal 4:
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
26
& 0 oF . & 0 oF
EO OG a Ge sh Deine selonuue ae souvreg | OL 6L PL “*"******* sjosuop ur poyseaut ‘puny oy} wo spusprary
0 OF e& “*""**"**"osn 84,0108 oy} tox adoosoxorpY ¥ Jo oseyorng | G 9 BG “TTT “Oggy kxenute T “sroyueg 30 eouR]eiL
12 &e ‘SINAWAV J YE 2 "SLA AON,
WNNOOOYW GSAUT, (GNA NOSAWVP-MOTUVG ,,
9 8 OGIF 9 8 OGLE
9 OL Tg C7 ees "" OBST ‘90(T Te “stoyueg 48 course 0 CT 89 BESS Rae eR ee 9 eee care ® he SOTTO
OR eee spoiouant> ay 101, &6 aed g uvptpodomeyy ul poyseaut pun, oy} Wo spueprary
UOC epony (yr “suedn UyOr apy 0} plVemMy | 9 SLTG “rte tts ses: QgeyT Arenuee [ ‘s1eyueg ye couvpeg
12 Gs ‘SINHA V J TD OB "‘SLAIGO MY
“ENNODOY ESoay, ,~AaNOWy TVOI01IOT+y TTAXT ,,
a seinamenininienaen
G VI 8oF G VIL 8oF
9 6 68 ‘"'"****¥Yo0Ig onquoqa “400 red F AVMTILIT UI9}S0 AA
OTRO TAGs rae 8 serine near "da Tg “stoyurg ev souvpeq YON pus wopuo'yT UL poJsoAUL puny oy} UO spueplal(T
OC ale se ee BpAW Yt ooprmouim STINGOT PIR TO) Gl sia oes e so * Qeay ATunuEry) © croueen qe couelecl
ie Ge "SINGNWAV 7D 1G? "SLdIG“OaYy
“ENOOOOW GSAUT, (INO IVOINOIOTH NosIHoONaTy ,,
a GLE G &L 6oF
J, CT Te ets t ess" Oger 0q@ Te ‘sioyueg 4e cowereg -
O OL OL e9iqneq “wv ‘JOLT OF POplVM [VpoPy Ploy suryiays Jo yoo 4 GI Tg ° ‘s}ueg sod ¢ poonpory ur poyseAut pun 7 94} UO SpuoprlAl(y
OL 9 6 ee cor nv ey, FeO pI OL 9L TE “occ: Egyy Arenuve 7 ‘sxeyueg 4v oouvpeg
(G3 ‘SLNGIWAV 7 Usimte: ‘SLaIGO ay
“ENQOOOW Gsauy, (GNA NOMLVNOG NOLSVTIO A, ,,
I
N
FINANCIAL REPORT.
0 0 GSt8F O 0 Ggh8F
OPO BOG e
OF Ga tie o
IT OT SLOT ¢
0 0 4002 0
wv
(sree) Se
OF 20 S962 eS
boG @ ttre
E208) 5. 2
eSe Oe
O 0 GPR tt ees es kgato0g oyy JO AoARy UT couRTeg
ps §F ‘SLaaq Vi AS te
"IS8T ‘927 GI
"sm04T ‘SRAUATAL NAMD ‘£
[ ‘secongponqng pjosun fo
YIOS pu ‘ainquung Lioiquvy ‘sworoapjog ay2
JO Anjor oYyZ apnjowe pow soop ancgn ay T, ‘IN|
‘(p00s peiopisuo0d) suorynqryu0D Tenuuy Jo SIVOLIW
"******(poos pexopIsuod) seej-uolsstuipy Jo savory
G 9801 “*** 86 38 ‘s}uep 10d ¢ poonpery
0 Op Ro 20 8 88 Sey tes CORIO)
Sa —: Ayrodorg pepun,y
rere" 0887 9° 1g ‘Spuvy syprerQ ur sourpeg
res" * OSSl ‘99 Tg ‘spuvy stoyuvg ur courpeq
‘(poos poxepisuos) Teummor 07 sieqirosqng WOLE ONT
sreeeeccsss dey JO Junos0v uo pxozueig wO0Ay end
C0800 00080 0 O50 OP0s0 00.0 090 O06 0-070 OD ON 050-0 DO “OY “TAXXX
‘JOA TwuMor Jo yunovse uo “og » UBULSUOTT WOLF ON
‘KLUGIOUg
"OSS ‘laquiasag: JsTe -AUUALOUd S ALTIOOG IHL TO NOILVA'TY A.
6 G GF
Se Se ed 6 6G 9 ‘*"***s}UeD Jed gE MENT UT pojsaAuT pun,y oy} UO spuoprary
(6) Fae DE PROD RD ae Bact OSST “9d Te ‘“stoxueg ye souryeg O GQ fitters teeseeees OSsT Atenuep 7 ‘sroyneg qv couepeg
[Do G3 “SINGTWAV I DSS "‘SLAIGO MY
“ENNOD0V LSQWT, «c GNOY AASOTG ,,
28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
AWARD OF THE WoLtAston MEDAL.
The Reports of the Council and of the Committees having been
read, the President, Roserr Eraerrmer, Esq., F.R.S., presented
the Wollaston Gold Medal to Prof. P. Martrmy Duncan, M.B.
Lond., F.R.8., F.G.8., and addressed him as follows :—
Professor Duncan,—
It is with no ordinary pleasure that the Council have awarded to
you the Wollaston Medal, the highest honour that it is in their
power to bestow, in recognition of the valuable services which you
have rendered during so many years to the advancement of Geology,
and especially of Paleontology; and I may add that it is equally
productive of gratification to me that this honour is to be formally
conferred upon you by my hands. Since the year 1863 paleonto-
logists have been indebted to you for no fewer than twenty-six
memoirs relating to the history, structure, and distribution of the
fossil Actinozoa, a group which you have made peculiarly your
own by long-continued and most careful researches. Further, you
have enriched the publications of the Paleontographical Society
with several most important treatises on the British Fossil Corals,
supplementary or, rather, perhaps, complementary to the classical
Monograph of MM. Milne-Edwards and Haime.
These labours alone, and the value of their results, might have
justified the Council in awarding you the Wollaston Medal; but
besides your researches upon the Actinozoa, we have to point to
several important papers upon the fossil Echinodermata, to others
relating to subjects of Physical Geology (also freely touched upon
in your more special memoirs), and particularly to your exceedingly
important work in connexion with the Geological Survey of India,
in describing the fossil corals of that Peninsula, and discussing the
questions of both zoological and geological interest which naturally
arise out of the study of those organisms. Few, mdeed, of our
Fellows are in a better position to appreciate your valuable labours
than myself; scarcely a day passes that I have not occasion to
consult one or more of your contributions; and the more I consult
them the more I am convinced of their value. Patiently and un-
obtrusively, for nearly twenty years, you have followed out the
line of research necessary for the fulfilment of your self-imposed
task; you have sacrificed the advantages of professional life to
devote your energies to the advancement of science; for seven
years (from 1864 to 1870) you gave the Society the benefit of your
services as one of its Honorary Secretaries, and for two years
(1876, 1877) you worthily occupied the Presidential Chair. Such
considerations as these would not alone, perhaps, have warranted
the award of the Council; but the recollection of such services
rendered to the Society is hardly out of place, as supplementing
those more generally appreciable merits upon which the award was
ANNIVERSARY MEETING—-MURCHISON MEDAL AND FUND. 29
really founded. On all accounts it is with much pleasure that I |
hand to you the Wollaston Medal.
Professor Duncan, in reply, said,—
Mr. PrustpEnt,—
The gift which you have presented to me, in the name of the
Geological Society, I receive with feelings of great respect and
thankfulness. ‘This Medal comes to me bringing a twofold pleasure ;
for it is a distinction which has been hallowed and ennobled from
its reception by a long succession of illustrious men, amongst whom
were the founders of our science, our teachers, and many of our
best friends ; and because, in presenting it to me, you have spoken
so sympathetically in appreciation of my scientific work—work
which I have been enabled to bring before the world in consequence
of the advantages which this Society has placed within my reach.
Cheered by this expression of your approbation, I shall labour on
in this our common and much-loved science, endeavouring always
to merit the esteem of the Fellows of this Society.
AWARD oF THE Murcuison MeEpAt.
The Presipent then presented the Murchison Medal to Prof.
_ ArcuipaLp Gernie, F.R.S., F.G.S., and addressed him as follows :—
Prof. Gerx1E,—
If any one Fellow of our Society more than another could be
selected to receive the Murchison Medal for his valuable contri-
butions to Geology, it would be yourself; since no man living has
contributed more to the advancement of that science which it is the
special object of our Society to cultivate and diffuse. Your labours
in the field connected with your duties as Director of the Geolo-
logical Survey of Scotland, your learned and valuable contributions to
the Journal of our Society, the Transactions of the Royal Society
of Edinburgh, the Glasgow Geological Society, and other pub-
lications too numerous to mention, eminently qualify you to be the
recipient of the Medal founded by your late chief and friend Sir
Roderick Murchison. To enumerate your contributions to the
literature of the geology of Scotland, or your many important
writings connected with our science, would lead me too far
—some thirty papers, besides educational works, have resulted
from your industry and knowledge. Your able paper on the “ Old
Red Sandstone of Scotland,” published in the Transactions of the
Royal Society of Edinburgh, would of itself entitle you to the highest
consideration of the Society. Able, indeed, are other contributions,
especially those “On the Chronology of the Trap Rocks of Scot-
VOL. XXXVII. d
30 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
land,” “On the Date of the last Elevation of Central Scotland ” (in
vol. xviii. of our Journal), ‘‘On the Phenomena of Succession
amongst the Silurian Rocks of Scotland” (Trans. Glasgow Geol.
Soc. vol. ii.), and “ On Earth Sculpture.” The Council believed,
too, that it weuld be gratifying to you to receive as a mark of their
esteem and sense of your untiring labours, the Medal founded by
one with whom in earlier life you were closely associated, and
whose endowed Chair of Geology in the University of Edinburgh
you have been the first to fill.
Prof. Grrcin, in reply, said,—
Mr. PREsIDENT,—
If any thing could add to the gratification with which I receive
this honour from the Geological Society, it would be the very kind
and flattering terms in which you, Sir, have made the award, and
the Fellows have been pleased to receive the announcement. The
Geological Society of London has always seemed to me to be truly
the Geological Society of the British Empire, electing its Fellows
and bestowing its rewards, not in a local, but in a truly catholic and
generous spirit. This conviction was renewed and strengthened in
my mind on receipt of the unexpected intimation of the bestowal of
one of the Society's Medals upon myself, as my contributions to
science have but rarely appeared in the Society’s publications, and
I am so seldom able to be present within the Society’s walls. I
receive the Medal with peculiar pleasure ; first, as a valuable mark
of the Society’s recognition, and next, as another link of association
with the memory of Murchison, which is one of the most precious
possessions of my life.
AWARD oF THE LYELL MEDAL.
The Prestprent next handed the Lyell Medal to Mr. Wartneron
W. Suyre, F.R.S., F.G.S., for transmission to Dr. J. W. Dawson,
F.R.S., F.G.8., of Montreal, and addressed him as follows :—
Mr. Warineton SuytH,—
Sir Charles Lyell, in founding the Medal that bears his name,
intended that it should serve as a mark of honorary distinction,
and as an expression on the part of the governing body of the
Society of their opinion that the Medallist has deserved well of
science. I need hardly say that the Council, in awarding the Lyell
Medal to Principal Dawson, have done so with a sincere apprecia-
tion of the high value of his truly great labours in the cause of
Paleontology and Geology. When I refer to his published papers,
I find that they number nearly 120, and that they give the results
of most extensive and valuable researches in various departments of
geology, but more especially upon the paleontology of the Devonian
ANNIVERSARY MEETING-——-LYELL MEDAL AND FUND. 31
and Carboniferous formations of Northern America. No fewer than
30 of these papers have appeared in the pages of our own Quarterly
Journal. Considering the nature of these numerous contributions,
the Council would have been fully justified in awarding to Dr.
Dawson one of its Medals, upon the sole ground of the value of their
contents ; but these are far from representing the whole of the results
of his incessant activity in the pursuit of science. His ‘ Acadian
Geology, ‘ Post-pliocene Geology of Canada,’ and ‘ Fossil Plants of
the Devonian and Upper Silurian of Canada’ are most valuable con-
tributions to our knowledge of North American Geology ; whilst in
his ‘ Archaia,’ ‘The Dawn of Life,’ and other more or less popular
writings, he has appealed, and worthily, to a wider public. We are
indebted to his researches for nearly all our knowledge of the fossil
flora of the Devonian and other Precarboniferous rocks of America,
and of the structure and flora of the Nova-Scotian coal-field; and,
finally, I must refer especially to his original investigation of the
history, nature, and affinities of Hozoon. These researches are so
well known that they have gained for Dr. Dawson a world-wide
reputation ; and it is asa slight mark of their esteem, and their high
appreciation of his labours, that the Council have awarded to him
this Medal, which I will request you to forward to him, with some
verbal expression of the feeling with which it is offered.
Mr. Warineron W. Suytu, in reply said—
That it gave him much pleasure to receive this Medal for Dr.
Dawson, who much regretted that he was unable personally to be
- present, but had addressed a letter to the President expressing his
sense of the honour conferred upon him, in the following terms :—
*“[ regret that distance and the claims of other duties prevent
me from appearing in person to express to the Geological Society
my sense of the honour conferred upon me by the award of the
Lyell Medal.
“This expression of approval on the part of those whose good
opinion I value so highly is doubly grateful to one who is so deeply
sensible of the imperfection of scientific work done in circumstances
of isolation from the greater centres of scientific life, and under the
pressure of the severe demands made in a new and growing country
on those engaged in educational pursuits.
“Tt is further especially gratifying to me that this token of your
kindly recognition is connected with the illustrious and honoured
name of Sir Charles Lyell. Forty years ago the foundation of my
geological education was laid by the late Prof. Jameson and other
able educators in natural science, his contemporaries, in Edinburgh ;
but in so far as I have been able to build any thing worthily on
this substructure, the credit is due to the study of the ‘ Principles
of Geology, and to the personal friendship and generous kindness
of Sir Charles Lyell more than to any other cause.”
32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
AWARD oF THE Biespy MEDAL.
The Presrpent then handed the Bigsby Medal to Prof. Morris,
F.G.S., for transmission to Dr. Cuartrs Barrors, and addressed him
as follows:
Prof. Morr1s,—
The Council of this Society have selected Dr. Charles Barrois to be
the recipient of the Bigsby Medal, and have awarded it to him
for his numerous papers and contributions to geological science.
Dr. Barrois’s chief or most important work (written in the year
1876, and published at Lille) is entitled ‘ Recherches sur le terrain
erétacé supérieur de l’Angleterre et de l'Irlande,’ a production almost
exhaustive in its description of the Cretaceous rocks of England
and Ireland, and of the utmost value to English students of
geology. Dr. Barrois in this work has been the first to attempt to
arrange the English Cretaceous rocks in Paleontological zones, and
eminently has he succeeded in defining and correlating the horizons
of France and Britain. He is also the author of a ‘ Mémoire sur
le terrain crétacé du Bassin d Oviedo, Espagne,’ with a paleonto-
logical description of the Kchinodermata by Gustave Cotteau. His
great industry and untiring zeal for geological science entitle him
to the consideration of the Council; and I therefore beg you to for-
ward to him the Bigsby Medal as our recognition of his services,
and, according to the wishes of the founder, we look forward to
other and equally valuable contributions.
Prof. Morris, in reply, said :—
Mr. PRESIDENT,
I have much pleasure in receiving the Bigsby Medal for transmis-
sion to Dr. C. Barrvis in recognition of his labours for the promotion
of geological science. I feel assured that while he will fully appre-
ciate the award, it will be also satisfactory to his geological col-
leagues in the north of France, and especially to that energetic and
accomplished geologist, Prof. Gosselet, under whose tuition and en-
couragement he has been partly stimulated to prosecute those
researches which have this day been recognized by the Council of
the Geological Society.
Not only, Sir, as you have justly stated, has Dr. Barrois contri-
buted to our knowledge of’ the physical and paleontological con-
ditions of the Cretaceous rocks of the north of France and of this
country, but among other researches he has been occupied with the
Paleeozoic strata of Brittany and also of Northern Spain, on which
latter, he informs me, a memoir will shortly be published. In con-
lusion I may read the following extract from a letter received from
Dr. C. Barrois, who regrets exceedingly that a previous engagement
rendered it impossible for him to express personally his grateful
sense of the honour done to him by this award. He says :—
ANNIVERSARY MEETING——-WOLLASTON FUND. 33
‘Will you please present my best thanks to the Society for
having judged my labours for the advancement of geological science
worthy of the Bigsby Medal.
“Tt is a great and quite unexpected honour for me to have my
name on the list of all the good geologists who have received the
Medals of the old and illustrious London Geological Society. By
the award of the Bigsby Medal I feel myself honoured in the highest
degree, as nothing can be more precious to a scientific man than
the recognition of his endeavours by the masters and leaders of his
own special science. I was already greatly indebied to English
geologists as having so often used and profited by their works during
my travelsin Great Britain. I now incur a new debt to them, as
the Bigsby Medal conferred upon me is given, according to the
donor’s bequest, ‘to those not too old for further work.’ Iam thus
mightily stimulated to work for the performance of my duty ; I will
endeavour to discharge it and to become worthy of so high an en-
couragement.”
AWARD OF THE WoLLASTON DoNATION Funp.
In handing to Prof. J. W. Jupp, F.R.S., Sec. G.S., the balance of
the Wollaston Donation Fund for transmission to Dr. Ramsay H.
Traquair, F.G.S., the Presrpznt said :—
Professor J upp,—
In handing to you, to be forwarded to Dr. Traquair, the balance.
of the proceeds of the Wollaston Donation Fund, I have to request
that you will inform him of the feeling of the Council, that it is
rarely that they can have the opportunity of awarding this fund to
a more able and accomplished naturalist than himself. Huis long-
continued researches upon the Ganoid Fishes of the Carboniferous
formation have rendered his name eminent in this department of
Paleontology. As an accomplished anatomist and zoologist, we
must have every confidence that his treatment of these Vertebrates in
the memoir which he is contributing to the publications of the
Palzontographical Society will be of the most careful and judicious
description, whilst the value of this and his other works is vastly
enhanced by the beautiful figures with which he illustrates them.
Under these circumstances it affords me much pleasure to place in
your hands, for transmission to Dr. Traquair, the balance of the
Wollaston Fund, which I hope he will receive as some recognition
on the part of the Society of the value of his researches, and, at the
same time, as a small aid to him in further prosecuting them.
Prof. Jupp, in reply, read the following communication, received
from Dr. Traquair —
“Mr. PresiDENT,—
“Permit me cordially to thank the Geological Society for the
34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
honour which it has conferred upon me by adding my name to the
list of those who, in former years, have received this award.
“Tf the subject of Fossil Ichthyology is not only fascinating, but
essential to the student interested in the great problems of Verte-
brate Morphology and Descent, it cannot fail also to be of import-
ance to the geologist, who, calling to his assistance every available
branch of natural knowledge, seeks to arrive at a scientific concep-
tion of the past history of the earth and its living inhabitants. It
is, therefore, very gratifying to me to receive from the Geological
Society of London this very unexpected token of sympathy and
recognition, considering that the amount of work which I have been
able to achieve in this field is as yet comparatively small. It will,
however, stimulate me to further exertions; for the field is itself a
large one, and in spite of the magnificent labours of Agassiz and
the accumulated researches of many other writers, still affords room
for plenty of work.”
AWARD oF THE Murcuison GrotoeicaLt Funp.
The PrestpEnr next presented the balance of the proceeds of the
Murchison Donation Fund to Franwx Rvurzey, Esq., F.G.8., and
addressed him in the following words :—
Mr. Ruritzy,—
For many years you have devoted your time and attention to the
microscopical structure of rocks and rock-forming minerals, a branch
of scientific research of the highest importance to the petrologist
and geologist; and now that our attention is being so much drawn
to the structure of the metamorphic and igneous rocks, with a view
to a better nomenclature and a revision of old and obsolete views,
the Council of our Society believed that in your hands good work
would still be carried on; they, therefore, have awarded to you
the balance of the Murchison Fund, which I have much pleasure in
handing to you in recognition of your past researches, the results of
which you have from time to time communicated to the Journal of
the Society. Few are more aware than myself of the interest you
take in this branch of study, and it affords me much gratification
to be the medium of conveying to you the appreciation of the Council
and the accompanying fund.
Mr. Rurtry, in reply, said that he felt deeply the honour thus
conferred upon him, which was additionally gratifying to him per-
sonally, as it was associated with the name of a former distinguished
Director-General of the Geological Survey. With regard to his own
special work, to which the President had alluded in such kind terms
of praise, he remarked that in all such work the investigator is
particularly liable to fall into error, and that all special microscopical
researches upon petrological subjects need to be constantly checked
by observations in the field. It was a further gratification to him
to receive the award of the Council, for which he wished to express
ee ee eee
ANNIVERSARY MEETING——-LYELL FUND. 35
his gratitude, from the hands of an old teacher, to whose instructions
he was indebted for the habits of minute and careful investigation
inculcated in his lectures.
AWARD oF THE LYELL GroLogicaAL Funp.
In presenting to G. R. Vinu, Esq., one moiety of the balance of
the proceeds of the Lyell Donation Fund, the President addressed
him as follows :—
Mr. Vinzt,—
A moiety of the balance of the proceeds of the Lyell Geological
Fund has been awarded to you by the Council of the Geological
Society. In making this award the Council were actuated in part
by the wish to express their sense of the value of your researches
upon the fossil Bryozoa of the Paleozoic rocks, as evinced especially
by your published writings on the Diastoporide, an exceedingly
dificult group, and in part by their desire to assist you in the
further prosecution of your investigations. I have much pleasure
in handing to you this small testimony of the appreciation of the
Council.
Mr. Vins, in reply, said :—
Mr. PrrstpEnt,—
I receive through you this token of recognition, on the part of the
Council, of my humble labours, with mingled feelings of pleasure
and pride. I cannot, at present, understand the reason why I
should be selected as one of the recipients of the Lyell Fund. It
cannot be for what I have done for science ; for, as yet, my name is
young; it must be that, having looked upon my labours with favour,
the Council desires to stimulate me to further exertions. If such be
the motive, I shall do my utmost to fulfil the higher promise which
my hitherto crude efforts have awakened. When, some years ago, I
began to study the Carboniferous Polyzoa, I wrote to Prof. Duncan,
F.R.S., asking for certain information respecting these Polyzoa; he
wrote me back word saying that he did not know much about the
species himself, and he did not think that there were many men in
England who did; but he counselled me to go to work and find out
for myself, and then he and others would be glad to know. Accept-
ing this advice, I set to work, with results which you and the
Council so kindly acknowledge to- day by this award.
From your hands, Mr. President, I feel also proud in accepting
the award. Many years ago, when poor and unknown, I sought
information on this and other things from the cases of the Museum
of Practical Geology. On that occasion you helped me by word and
deed to name my private series of fossils—a kindness on your part
that I never have forgotten or shall forget.
36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
To the Fellows of the Geological Society I also tender my thanks
for the manner (judging by the discussions which have followed the
reading of my papers) in which they have received my criticisms on
a most difficult group of fossils. I may differ from many of you in
the future, but I shall hope to do so in such a manner as to show
that I do not forget that we are fellow-students and at the same
time gentlemen.
The PresipEent then handed to Prof. H. G. Szerezy, F.R.S., F.GS.,
for transmission to Dr. Anton Frirson, of Prague, the second moiety
of the Lyell Donation Fund, and said :—
Professor SEELEY,—
The Council has awarded a portion of the Lyell Geological Fund
to Dr. Anton Fritsch, Professor of Zoology in the University of
Prague, in recognition of his valuable contributions to paleontology.
Dr. Fritsch is an accomplished zoologist, who has enriched his:
studies of many groups of fossils, invertebrate and vertebrate, with
admirable knowledge of existing life. During the last thirty years
Dr. Fritsch has published about one hundred and twenty memoirs,
many of which relate to paleontology and geology. Besides scattered
papers on Hozoon, Callianassa, and other subjects connected with the
fossil fauna of Bohemia, Dr. Fritsch has also published some standard
works monographing the fossils of his native land. These comprise
memoirs on the Cretaceous Cephalopods (1872), the Cretaceous Rep-
tiles and Fish (1878), and his great work on the Fauna of the Per-
raian Rocks (still in progress), of which two volumes, devoted to Am-
phibia, have been issued. ‘These volumes are excellent examples of
descriptive work, illustrated worthily, and this award is especially
intended to mark the sympathy of the Council with Dr. Fritsch in
his endeavours to adequately make known the Permian fauna, and
in the hope that the fund may assist him in completing a work which
has already taken high rank among paleontological monographs.
Prof. SEELEY, in reply, said :—
Mr. PrestpEnt,—
Dr. Fritsch will, I believe, appreciate the honour of the award
which you have made, no less than the words in which you have ex-
pressed the esteem in which his work is held in this country. I
have seen the materials upon which his studies of the Amphibia are
founded, and doubt whether any more important work has been
done in paleontology during the past year, or whether it could have
been accomplished at all by any one less skilled in the methods of
zoology than Dr. Fritsch. His enthusiasm for research has given
to his works a wealth of illustration that will help materially in the
advance of knowledge, while by electrotyping the specimens he has
rendered them easily available for study by all anatomists. I shall
have great pleasure, Mr. President, in informing Dr Fritsch of the
kindly way in which your award has been received by the Society.
ANNIVERSARY ADDRESS OF THE PRESIDENT. iy)
THE ANNIVERSARY ADDRESS OF THE PRESIDENT.
Rosert HruEriver, Hsq., F.R.S.
In accordance with the usual practice, 1 must commence my
Address with brief Obituary Notices of some of the more promi-
nent Fellows and Members of the Society whose loss we have
had to deplore since the last Anniversary Meeting.
SEARLES VALENTINE Woop, born Feb: 14, 1798, died Oct. 26,
1880. He became a Fellow of the Geological Society in 1839.
Mr. Wood was born on St. Valentine’s day; hence his name.
He went to sea as a midshipman in the ‘ Thames’ (one of the East-
India Company’s mercantile fleet) in 1811, and continued in that
service until the year 1826, when, being disappointed in obtaining
the command of a ship that had been promised him, he retired
from a maritime life and devoted himself to paleontological
studies. Settling in his native place in Suffolk, he gave the
larger part of his attention to the Crag: but he also collected ex-
tensively from the Hampshire Tertiaries ; and for the purpose of
working out the relations of these to the beds of the Paris basin,
he formed an extensive collection of the French Eocene Mollusca.
From these materials, and from correspondence with Deshayes
and other French savans, he was prepared to have taken up the
description of the English Eocene Mollusca long before he actually
did so, circumstances having determined his undertaking the de-
scription of the Mollusca from the Upper Tertiaries first. He
also formed a considerable collection of recent Mollusca for com-
parison in working out the relations of the Mollusca from Tertiary
formations. Having left Suffolk from ill health, and settled in
London, he was in 1837 introduced to Sir Charles (then Mr.)
Lyell, and was associated with him in the endeavour in which
Lyell was then mainly engaged, to work out a better knowledge of
the Tertiary formations, which up to a period not long before that
time had been regarded as of small account in comparison with
the “Secondary” group. In this task Lyell relied principally on
S. V. Wood and the late G. B. Sowerby for the determination of
the identity of the Molluscan remains from various countries with
those found fossil in England, and with the Molluscan fauna lying
in existing seas, so far as these were then known. Mr. Wood
also, for a few months about this time, acted as Curator of the
Museum of the Geological Society.
Urged to the task by Lyell, he commenced (with the coopera-
tion of the present Mr. G. B. Sowerby as engraver and intended
publisher) the description of the ‘ Crag Mollusca; ’ and considerable
progress had been made with the manuscript and plates of the
first or “ Univalve” part of this work, when the Paleeontographical
Society was formed, in 1847; this part formed the first volume of
the magnificent series of scientific publications which have been
VOL. XXXVII. @
38 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
issued by that Society. The rest of the ‘ Crag Mollusca’ followed
in subsequent years ; and upon the completion of this work, and in
recognition of his labours generally in connexion with the Tertiary
Mollusea, the Council of the Geological Society awarded to Mr.
Wood in the year 1860 the Wollaston Medal. A large supple-
ment to this work, embodying the discoveries which had subse-
quently accumulated, was prepared by Mr. Wood; and this, ac-
companied by an introduction describing geologically the formations
from which the remains embraced by the work had been obtained,
from the pen of his son and of Mr. F. W. Harmer, was issued by
the Paleontographical Society in 1871 and 1873. <A second sup-.
plement followed this in 1879; and Mr. Wood was actively en-
gaged, up to the day of his seizure with fatal illness, on another
small addition. On the completion of the description of the Mol-
luscan remains from the Crag, Mr. Wood presented the unrivalled
collection of them, which he had been forming during thirty years,
to the nation, in order that, by being preserved intact in the
British Museum, the types of all the forms which had been de-
scribed and figured by him in his work (save two or three which
belonged to other persons) might be available for examination and
comparison by naturalists engaged in similar labours.
He also presented to the nation the valuable collection of ver-
tebrate remains (including among them the unique jaws of Alligator
hantomensis and Microcherus erinaceus) which he had, in 1843-5,
extracted from the Hocene Freshwater beds of Hordle Cliff,
from which beds up to the time when he commenced forming this
collection no such remains had been known. These he partially
fioured and described in the London Geological Journal; but the
stoppage of that publication brought this part of his labours to an
unexpected termination. In 1858, having the advantage of an
unrestricted manipulation of the more extensive collection of
Eocene Mollusca which had been formed by his friend F. E.
Edwards, he commenced the description of the Hocene Bivalvia,
Mr. Edwards taking upon himself (and having commenced before
this) the Cephalopoda and Gasteropoda. Several parts of this
work were issued by the Paleontographical Society. Failure of
health put a somewhat premature period to Mr. Edwards’s share
in this work ; but Mr. Wood continued his labours for some years
longer, relinquishing them only when, shortly before Mr. Edwards’s
death, his collection was acquired by the British Museum. During
the time in which it remained in Mr. Edwards’s possession he was
accustomed to place in Mr. Wood’s care, for study at his leisure,
all specimens he possessed which in any way illustrated the subject
in hand; but this the transfer of the collection to the British
Museum rendered impracticable ; and as it was Mr. Wood’s feeling
that, in addition to that opportunity for careful study, all forms as
to which any doubt existed ought to be carried abroad and com-
pared with those in the museums of France and Belgium, if justice
was to be done to the subject, and as at his advanced age he was
unable to accomplish this, he on the issue of the part in the volume
ANNIVERSARY ADDRESS OF THE PRESIDENT. 39
of the Paleontographical Society for 1870 relinquished the further
prosecution of the ‘ Hocene Bivalvia,’ although he subsequently
added a small contribution (both to Mr. Edwards’s and his own
portion) on special groups of Eocene Mollusca, which he was able
to do from resources afforded by his own collection and the collec-
tions of some friends.
He maintained his activity both of mind and body up to the
day of his seizure with fatal illness, which took place on the 21st
and terminated with his death on the 26th of October last. He
was buried in the churchyard of Melton, near Woodbridge, in
view of the Crag of which the study had occupied so much of his
life.
JOHN JEREMIAH BiasBy, M.D., F.R.S., one of the oldest of our
Fellows, and a man endeared to all who knew him by many amiable
qualities, died at his residence in Gloucester Place on the 10th
February in the present year. He was theson of Dr. John Bigsby,
and was born at Nottingham on the 14th August, 1792; so that at
his death he was in his 89th year.
Deciding to follow his father’s profession, he took his degree
of Doctor of Medicine at Edinburgh; and soon afterwards he
must have entered the military service, as, from a chance note
in one of his books, it appears that he was at the Cape in 1817.
In 1818 or 1819 he went to Canada as the Medical Officer to a
large detachment of a German Rifle Regiment in the British
Service; and in Canada he remained for several years performing
a variety of commissions intrusted to him by the Government.
Thus in the summer following his arrival in the Colony he was
sent to the Hawkesbury Settlement, where a severe epidemic of
typhus fever had broken out among the miserable Irish immigrants ;
and in the next year his marked taste for Geological studies led
to his being commissioned to travel through Upper Canada and
make a general report upon its Geology. In 1822 he was ap-
pointed British Secretary and Medical Officer to the Boundary
Commission, which had already been in existence for three or four
years. In the journeyings to and fro necessitated by these em-
ployments Dr. Bigsby had many opportunities of making himself
acquainted with the geological phenomena of regions then very
little known ; and it is chiefly to these that his published papers
relate. In 1823 he was elected a Fellow of this Society.
He appears to have returned to England about the year 1827,
and then proceeded to practice his profession at Newark in Not-
tinghamshire, remaining there until 1846, when he came to London,
where he afterwards resided until the end of his life. R
Dr. Bigsby was elected a Fellow of the Royal Society in 1869,
and received the Murchison Medal from this Society in 1874.
His published papers are about twenty-seven in number; the
earliest, entitled, ‘‘ Remarks on the Environs of Carthage Bridge,
near the mouth of- the Genesee river,’ appeared in Silliman’s
American Journal in the year 1820. It was followed by several
e2
40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
other papers on geological subjects in the same periodical. In
1823, the year of his election, he forwarded a paper to this Society
‘“*On the Geography and Geology of Lake Huron,” which was
published im 1824, in the first volume of our ‘Transactions.’
Until his return to England his contributions to scientific litera-
ture made their appearance chiefly in American publications ; and
for some years after his return he seems to have done but little,
his medical practice probably occupying his time very fully. After
his removal to London, however, several papers from his pen were
communicated to the Society ; and among them may be noticed
especially his paper ‘“‘ On the Paleozoic Basin of the State of New
York,” which appeared in the Quarterly Journal for 1858, and
was followed by “An Inquiry into the Sedimentary and other
Natural Relations of the Paleozoic Fossils of the State of New
York,” published in 1859; his note “ On the Erratics of Canada,”
printed in the Journal for 1851; and his last communication to
our ‘ Proceedings,’ ‘‘On Missing Sedimentary Formations,” pub-
lished in 1864. Other memoirs of his appeared in various perio-
dicals, such as the ‘ Philosophical Magazine’ and the ‘ Annals and
Magazine of Natural History,’ the last of them bearing date 1867.
The narrative of his Canadian travels appeared in 1850, in two
octavo volumes, under the fanciful title of ‘ The Shoe and Canoe,’
Although evidently written by the light of knowledge subsequently
obtained, it furnishes an interesting-account of the condition of
Canada some sixty years ago, and is renderedamusing by the dis-
play of that naive geniality mingled ‘with ‘shrewdness which cha-
racterized the author to the end of his life. It contains many
scattered popular notes on geological and other natural-history
subjects.
During the last twenty years of his life Dr. Bigsby was engaged
in a work of great labour and research, the first outcome of which
was the ‘Thesaurus Siluricus,’ published, with the aid of a grant
from the funds of the Royal Society, in 1868. It is a list of
described Silurian fossils, classified both zoologically and in accord-
ance with their distribution in time; and although, no doubt, errors
and defects may be detected in it, it will remain for a long time a
most useful aid to the student of Silurian Paleontology, and a
monument of the untiring industry of its author.’ The’ same
things may be said, perhaps in still stronger terms, of ‘a ‘second
publication of the same nature, the ‘Thesaurus Devonico-Carbo-
niferus,’ which appeared in 1878, a wonderful example of industry
and research in a man eighty-five years old; and not content with
these labours, Dr. Bigsby, to the close of his life, was hard at work
upon.a Permian Thesaurus, the MS. of which is left in an ad-
vanced state. The last books borrowed for the compilation of this
work were only returned to the Society’s Library when Dr. Bigsby
took finally to his bed.
The memory of our late lamented Fellow will be worthily kept
alive by the Medal which he founded in the year 1877. The
greater part of Dr. Bigsby’s fortune having accrued to him by
ANNIVERSARY ADDRESS OF THE PRESIDENT. 41
marriage, he gave himself only a life-interest in it, and decided
that the whole amount at his decease should go to the relations of
the ladies whom he had married and survived. Hence, from de-
lhieacy of feeling, he decided that instead of bequeathing a sum of
money to the Society for the purpose of founding a Medal, he
would provide the necessary funds out of his income during his
life ; and accordingly, in the above year, he gave the Society a sum
of money the interest of which was to be devoted to providing a
Medal to be given biennially, preferentially to those who had studied
American geology, with the further stipulation that the receiver
should be not more than forty-five years old, and *‘ thus probably not
too old for further work, and not too young to have done much.”
At first the Medal was to have been of bronze and accompanied by
a sum of money, the balance of the proceeds of the fund; but
subsequently the founder increased the amount of his donation suf-
ficiently to enable the Council to give a Gold Medal. In 1877 the
Medal was awarded to Prof. O. C. Marsh, and in 1879 to Prof. E.
D. Cope; this year it goes to Dr. C. Barrois.
Rev. James Crirron Warp. The announcement of the death
of Mr. Ward must have been to most of his many friends wholly
unexpected, both on account of the early age at which he passed
away, and the very brief illness which preceded his decease.
After a weakly boyhood he entered the Royal School of Mines
as a student in 1861, entirely through my suggestion, and gained
the Edward Forbes Medal and prize of books in 1864. In the
following year he joined the Geological Survey, and was sent down
to Yorkshire. He worked there on the Millstone-grit and Lower
Coal-measures in the neighbourhood of Sheffield, Penistone, Hud-
dersfield, Halifax, and Leeds. Though Ward was never of robust
appearance, he obviously improved in health after leaving the School
of Mines ; so well did the laborious but healthy work of the Survey
agree with him.
In 1869 he was transferred to Keswick ; and the change from a
colliery district to a locality not only devoid of coal-pits, but one
in which wild Nature puts forth all her charms, was in the highest
degree pleasing to him. At Keswick his activity became twofold.
His Survey work and its results are now represented by his Geo-
logical Survey memoir on the Geology of the Northern part of
the English Lake District (published in 1876), and by numerous
maps and sections. He also contributed to the Geological Society,
and to various periodicals, many papers bearing on the structure
of the Lake Country. Of these may be mentioned, in the first
place, two on its glaciation, entitled, “The Origin of some of the
Lake Basins of Cumberland ” (Quart. Journ. Geol. Soc. 1874), and
“The Glaciation of the Southern Part of the Lake District” &c.
(Quart. Journ. Geol. Soc. 1875). In both papers the origin of
the lakes is discussed ; and (as regards the English Lake country)
the original investigations of the author tend to confirm the views
so long held by Prof. A. C. Ramsay. ‘These papers are illustrated
42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
with sheets of sections of the highest interest and value; and to make
the work more complete, the results of a series of soundings care-
fully taken on most of the lakes by this indefatigable worker are
also given.
In the years 1875 and 1876, and more recently, microscopical
examination of the rocks of the Lake District occupied much of
his time. Of papers on this subject I may here note one “On
the Granitic, Granitoid, and Associated Metamorphic Rocks of
the Lake District,” the first part of which appeared in the Quart.
Journ. Geol. Soc. for 1875, and the second in the volume of the
same periodical for 1876. Another paper is entitled, ‘“ Notes on
the Comparative Microscopic Rock-Structure of some Ancient and
Modern Volcanic Rocks,” and appeared in the Quart. Journ. Geol.
Soc. for 1875. Among his latest contributions to geological litera-
ture may be mentioned “ Notes on the Geology of the Isle of Man,”
which appeared in the Geological Magazine for January, 1880. The
following is by no means an exhaustive list of his productions :—
1. In 1868, “ Internal Fluidity of the Harth.” Geol. Mag. v.
p- 581, 582.
2. In 1869, “ Suggestions as to Geological Time.” Geol. Mag.
vi. pp. 8-13.
3. In 1869, “On Beds of supposed Rothliegende Age near
Knaresborough.” Quart. Journ. Geol. Soc. xxv. pp. 291-297.
4. In 1870, “On the Denudation of the Lake District.” Geol.
Mag. vii. pp. 14-17.
5. In 1871, “‘The Development of Land.” Geol. Mag. vin.
)0o TALS
6. In 1872, “On Rock-staming.” Geol. Mag. ix. pp. 389-391.
7. In 1873, “ On the Scenery of the English Lake District,
geologically considered.” Brighton, Proc. Nat. Hist. Soc. xx.
pp- 39-44.
8. In 1873, “On Rock-fissuring.” Geol. Mag. x. pp. 245-248.
9. In 1873, “ The Glaciation of the Northern Part of the Lake
District.” Quart. Journ. Geol. Soc. xxix. pp. 422-441.
10. In 1870, “* Coral Reefs and the Glacial Period.” Quart.
Journ. Sci. 1. pp. 170-178.
But the most characteristic side of his untirmg energy, and
perhaps its most important one, was the zeal with which he worked
for the diffusion of scientific knowledge while in Cumberland.
Before leaving Yorkshire he had written a small elementary book
on Physics ; and one of the firstfruits of his educational activity
at Keswick was a similar work on Geology, composed of nine
lectures delivered in the first place before a school audience, and
secondly before the Keswick Literary Society. Being simple,
clear, and free from unnecessary technicalities, his lectures soon
became popular, and the lecturer himself acquired influence.
As the originator and main support of the Cumberland As-
sociation for the Advancement of Literature and Science, and
of most of the local societies connected with it, he accomplished a
work which it may be hoped will not now be suffered to languish,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 43
but will remain a lasting monument of his beneficent activity. A
elance at the outer cover of the ‘ Transactions of the Cumberland
Association’ (Part IV. was published at the beginning of this
year) shows the date at which each of the associated societies was
founded, and discloses the fact that only one of them (at White-
haven) existed before Ward’s appearance in the county. The dates
of the others vary from Keswick 1869 to Silloth, the latest,
1879.
He married at the beginning of*the year 1877, and very shortly
aiter left the Lake country to do field-work in the lone barren
district of Bewcastle, on the Lower Carboniferous rocks, wintering,
however, in Keswick as before. But on finishing the Bewcastle
work he made preparations for taking Holy Orders, and was
licensed to the curacy of St. John’s, Keswick, in December 1878.
He was as successful in his new duties as he had been as a geo-
logical surveyor, and was appointed, at the beginning of last year,
to the vicarage of Rydal. But he was scarcely established in his
new home when a brief illness, which only at the last seemed
dangerous, caused his departure, at the age of thirty-seven years,
leaving behind him a widow and two children.
His genial disposition, and the absence in him of the least
approach to the temper of the dogmatist, caused him to number
among his friends men of every shade of speculative opinion. It
was this amiability, in addition to his ability as a lecturer and the
single-mindedness of his desire for the spread of knowledge, which
made him so successful in connexion with the Cumberland Asso-
ciation, when the simple fact of his not being a Cumbrian by birth
would have been fatal to any merely active and zealous man.
Davin Tuomas ANsTED was born in London on the 5th Feb- °
ruary, 1814, and, after education at a private school, entered the
University of Cambridge as a member of Jesus College. He was
32nd Wrangler in the year 1836, and proceeded to the degree ot
M.A. in due course in 1839. About four years afterwards he was
elected to a fellowship on the Ley Foundation of Jesus College,
which he retained for about eight years. In 1840 he was elected
Professor of Geology at King’s College, London, which office he
resigned in 1853. For some time, from 1845, he held the
Lecturership on Geology at Addiscombe, and was also Professor
of Geology at the College of Civil Engineers, Putney. From 1844
to 1847 he was Vice-Secretary of the Geological Society and Editor
of the Quarterly Journal. He became a Fellow in 1838. He was
elected to the Fellowship of the Royal Society in 1844. In 1868
he was appointed Examiner in Physical Geography to the Science
and Art Department.
By degrees his attention became diverted from the theoretic to
the practical aspect of his favourite study ; and for the last thirty
years of his life he acted professionally as a consulting geologist
and mining-engineer. For some time before his death he was in
failing health; and he expired on the 13th May, 1880, at his
residence, Melton, near Woodbridge, Suffolk.
44 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
Professor Ansted, however, when systematic teaching ceased to
be a part of his regular duties, did not abandon his interest in
geology as an educational subject, but not unfrequently lectured
and took part in examinations on this and allied sciences. His
pen also was rarely for long idle. He contributed three papers to
the Journal of the Geological Society, two of them containing
descriptions of remarkable mineral veins, published in 1856 and
1857; his third paper was upon the geology of Malaga and the
southern part of Andalusia (vol. xv. 1859). Besides these contri-
butions to the ‘ Quarterly Journal of the Geological Society,’
he published memoirs in:—the ‘Transactions of the Cambridge
Philosophical Society’ (vol. vii. 1842), “On a Portion of the
Tertiary Formations of Switzerland ;’ in the ‘ Annals and Maga-
zine of Natural History, “On the Zoological Condition of Chalk
Flints and the probable Cause of the Deposit of Flinty Strata
alternating with the Upper Beds of the Cretaceous Formation ”
(vol. xu. 1844), and other like publications. He was whole or
part author of a considerable number of volumes, the majority
of which were of a somewhat popular character ; and more than one
obtained a considerable share of success. He wrote lucidly
and pleasantly, whether upon matters directly scientific or upon
the incidents of travel. Among these works may be mentioned
the following :—‘ Geological Gossip,’ first published in 1860; ‘A
Short Trip to Hungary and Transylvania,’ in 1862; ‘ The lonian
Islands,’ in the year 1863; and ‘ The Great Stone Book of Nature,’
published in the same year. He also published a work on Geology,
in two volumes, in 1844, and more than one smaller book on this
subject, Physiography, or Geography. He was joint author (with
. Dr. R. G. Latham) of a work on the Channel Isles, and wrote,
in 1866, upon the Physical Geography and Geology of Leicester,
in the ‘ History of Leicestershire,’ entering largely into the litho-
logy and chemistry of the Charnwood rocks, as well as devoting
much space to their pure and speculative geology. In the Great
Exhibitions of 1851 and 1862 he contributed much to the ‘ Reports.’
His latest, and one of his most important works, was on Water
and Water Supply, published in 1878. Though for several years,
owing to pressure of business and the advance of age, he had
ceased to take an active part in the proceedings of many of the
scientific societies of which he was formerly an energetic member,
he did not lose that cordiality of manner and kindliness of dis-
position which have left a pleasant impression on the memory of
his friends.
In Wittram Hatnowrs Mirier, Professor of Mineralogy in
the University of Cambridge, our Society has lost a member who,
though never a contributor to our Journal, was among the most
eminent mineralogists in Europe, and the author of valuable works
and papers on that science. He was born April 6th, 1801, at
Velindre, near Llandovery, in Caermarthenshire, at which place his
father, Captain Miller, had a few years previously fixed his resi-
ANNIVERSARY ADDRESS OF THE PRESIDENT. 45
dence. The associations of the family were military, his father
having served through a part of the American war, by which he
had been a heavy loser, and other relatives having held commissions
and obtained distinction in the British army. W. H. Muller was
educated at private schools, and afterwards entered as a student
at St. John’s College, Cambridge, graduating in the year 1826,
when he was fifth among the Wranglers in the Mathematical Tripos.
In 1829 he was elected to a Fellowship at his College, and sub-
sequently proceeded to the degrees, first of M.A., and afterwards
(in compliance with the statutes by which it was then governed)
of M.D. ‘For some time he filled the office of a College Tutor ;
and his first literary work was a ‘Treatise on Hydrostatics,’ published
in 1831, and followed a few years subsequently by one on Hydro-
dynamics. At this time the chair of Mineralogy at Cambridge
was occupied by Dr. Whewell ; and under his guidance Mr. Miller
devoted himself to the study of Crystallography, with so much
success that, on the resignation of Dr. Whewell, he was elected to
the Professorship, the duties of which became the chief work of
his long and arduous life. In 1830 he was elected a Fellow of our
Society, and in 1838 a Fellow of the Royal Society. Six years
afterwards he vacated, by marriage, his Fellowship at St. John’s
College; but im 1874 he was again elected under the statute
(granted in 1860) empowering that Society to elect as Fellows
persons eminent for science or learning, though otherwise techni-
cally disqualified. Not long after this his health began to fail;
and in the autumn of 1876 a course of lectures, which he had
announced, was interrupted by a slight stroke of paralysis. This
proved the beginning of the end. He was never able to meet his
class again. Very slowly, but surely, his vital powers declined, a
torpor stealing alike over body and mind, until at last he fell
asleep on the 20th May, 1880.
Professor Miller’s name is inseparably connected with two im-
portant branches of scientific work. The first of these belongs, as
might be expected, to mineralogy. “Crystallography,” as has
been said by Professor Maskelyne, ‘was Miller’s science.” Other
workers, indeed, had preceded him in laying the foundation and
contributing important materials; but Professor Miller, ‘“ taking
the important memoir by Professor Whewell ‘ On the Geometrical
Treatment of Crystal Forms’ (published in the ‘Transactions of
the Cambridge Philosophical Society’), and Naumann’s treatise of
1823 (‘ Beitrage zur Krystallonomie’) as his starting-point, pro-
ceeded to develop a system of crystallography, which was not pub-
lished till 1838, but which was the most important work of his
life.” The especial feature of this book and of his labours in this
science ‘‘ consisted in working out into a beautiful system the
indicial method of notation and calculation in crystallography,
and obtaining expressions adapted for logarithmic calculations by
processes of great elegance and simplicity. Miller’s system, then,
gave expressions for working all the problems that a crystal can
present ; and it gave them in a form that appealed at once to the
46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
sense of symmetry and appropriateness of the mathematician.”
He thus, as it has been well said, ‘“‘ placed the keystone into the
arch of the science of crystallography ;” and the “future develop-
ment of that science, there can be little doubt, will follow on the
lines laid down by Miller.”
Professor Miller’s shorter communications on mineralogy and
physics are numerous and valuable, and; in addition to them and
to his original treatise, he published, in 1863, a tract on crystallo-
graphy. In 1852 a work appeared entitled a new edition of the
‘Elementary Introduction to Mineralogy, by the late William
Phillips, by H. J. Brooke and W.H. Miller. It is, however, no
_ disparagement to either the original author or his fellow editor to
say that Professor Miller made this volume almost his own.
But Professor Miller’s reputation does not rest only upon his
work as a mineralogist, great though that was. His name is no
less inseparably connected with the difficult and delicate experiments
and investigations connected with the restoration of the standards
of measurement and weight, and with the subsequent labours of
the International Metric Commission.
After the fire which, in 1834, consumed the Houses of Parlia-
ment, it was found that the standards of measurement and weight
were hopelessly ruined. Professor Miller was not a member of .
the Commission appointed to consider the questions connected
with their restoration, but lent the Commissioners much friendly
assistance. ‘Then, in 1843, a Committee was appointed to super-
intend the construction of the new Parliamentary standards of
length and weight, of which Professor Miller was a member ; and
to him was confided the construction of the new standards of
weight. In the ‘ Philosophical Transactions ’ for 1856 he describes
at length ‘the operations for restoring the value of the old
standard of weight, for constructing the new standard of a
different value, for constructing various derived standards, and
for establishing the relative value of the kilogramme,” a paper
which (to quote the words of the Astronomer Royal, indorsed by
a former President of the Royal Society, Sir Edward Sabine) “ will
long be cited as a model of accuracy.”
He was subsequently a member of a new Royal Commission for
“examining into and reporting on the state of the secondary
standards, and for considering every question which could affect
the primary, secondary, and local standards.”
In the year 1870 he was appointed a member of the “Commission
Internationale du Métre.”
He was appoimted Foreign Secretary of the Royal Society in
1856, a post for which he was eminently fitted by his accurate and
extensive knowledge of French, German, and Italian, his methodical
habits, and unvarying courtesy, as well as by his extensive scientilic
knowledge.
He received in 1865 the degree of LL.D. from the University
of Dublin, and in 1876 that of D.C.L. from Oxford. In 1870 he
was awarded a Royal Medal by the Royal Society. He was a
ANNIVERSARY ADDRESS OF THE PRESIDENT. A]
Knight of the Order of St. Maurice and St. Lazaro of Italy, and
of the Order of Leopold of Belgium. He was also an honorary
member of the Royal Society of Edinburgh and of numerous
foreign societies.
Three characteristics especially distinguished Professor Miller.
One was the remarkable extent, depth, and accuracy of his know-
ledge, not only on those questions which he had made peculiarly
his own, but also on all branches of physical science, only
equalled by the liberality with which he opened his rich stores
of learning to others, and especially to younger students. | Another
was the simplicity of his disposition. This, combined with a re-
markable inventiveness of mind, was shown even in his laboratory,
where the most homely odds and ends were utilized in the con-
struction of instruments capable of performing delicate measure-
ments. The third characteristic was the remarkable combination
which he exhibited of independence of thought and freedom of
opinion with gentleness of temper and speech, with forbearance,
courtesy, and respect for the opinion of others.
Blessed with much domestic happiness, and beloved by all who
knew him, he lived a tranquil and blameless life, devoted to earnest
work and the faithful performance of every duty, and passed away
lamented by a large circle of friends and admirers in this and other
countries.
Henry Luptam. We have to record the loss of Mr. Henry
Ludlam, F.G.S., who died on the 23rd of June, 1880, at the age
of 58.
Early a student of the natural sciences, Mineralogy became his fa-
vourite subject, in the cultivation of which he was greatly assisted by
the study of chemistry, which occupied many of the leisure ev ening
hours which the care of an important business allowed him.
Aided by an unusually critical judgment, he gathered together a
large and valuable collection of minerals, in which some of the
specimens were conspicuous for their perfection of crystalline form.
To these he subsequently added the well-known and important
collection which belonged to the late Mr. Charles Hamden Turner,
of Rooksnest, Surrey, and also that made by the late Mr. William
Nevill, F.G.S., of Godalming. The whole forms certainly the most
complete and probably the finest collection of minerals ever made
by a private collector.
But Mr. Ludlam was nota mere collector. He had long had
in view the desirability of preparmg a complete descriptive and
crystallographic catalogue of that which it had been his good
fortune to accumulate. This great work, to which he looked
forward as to a labour of love, was actually commenced by him
shortly before the illness which ended in his premature death.
Although Mr. Ludlam never contributed a paper to the ‘ Journal
of the Geological Society, he nevertheless took much interest in
its proceedings. His great liberality in the support of every thing
. bearing upon the kindred sciences to geology, and his munificence
48 PROCEEDINGS OF THE GEOLOGICAL SOCTETY.
as a collector possessing great knowledge of his subject, entitles
him to notice in the obituary list of our Fellows. He left by will
the whole of his superb collection of minerals to the museum in
Jermyn Street for the use of all students. It is now, therefore,
the property of the nation. Science, through the early death of
Mr. Ludlam, has lost an earnest student, while his personal friends
have to lament the loss of a warm-hearted and true English
gentleman.
Ropert CruTrersucK, F.G.S., was the eldest son of Robert
Clutterbuck, the historian of Hertfordshire. Mr. Clutterbuck was
educated at Harrow, being head boy of that School in 1817. He
entered as a commoner at Exeter College, Oxford, where, previous
to taking his degree, he gained University honours. He then
entered as a law student under the tuition of the late Sir William
Hayter. Mr. Clutterbuck spent some time on the continent, gain-
ing an unusual proficiency in the Italian and French languages.
During his residence at Watford he acted as a magistrate, and was
instrumental in raising funds for the restoration of the abbey
or.cathedral of St. Alban’s. As an author Mr. Clutterbuck
was well known through his works on the monsoons &c., and on
the rotatory action of storms; he also published accounts of
his journeys over the great desert from Aleppo to Bassora, and
the passage by Suez thr ough Egypt to determine the possibility of
an overland communication with India. Mr. Clutterbuck never
contributed to the ‘Journal of the Geological Society ;’ but he
wrote a paper on the Coprolite beds at Hinsworth, which was
published in the ‘Transactions of the Watford Natural History
Society, vol.1. 1878. He died September 15th, 1879.
Dr. Epwarp Meryon, F.R.C.P., F.G.S., &c., was many years
Fellow of the Geological Society, and some time member of the
Council, taking much interest in the working of the Society. He
never contributed any paper to the Journal. He, however, was the
author of several important works bearing upon his profession, among
which may be mentioned especially ‘The History of Medicine,’ ‘The
Physical and Intellectual Constitution of Man,’ ‘ The Functions of
theSympathetic System,’ and ‘ Practical and Pathological Researches
on the various Forms of Paralysis. Dr. Meryon was an accom-
plished and practical physician of great professional experience.
He was an accomplished scholar and true-hearted gentleman. Dr.
Meryon died November 8, 1880.
In Eriszan Watton, who died at his house near Bromsgrove on
August 25, 1880, in his forty-eighth year, the Society has lost an
artist who has been equalled by few, perhaps surpassed by none,
in his power of rendering faithfully the forms of mountains and
the structure of rocks. Huis studies of clouds and of the camel
prove the versatility of his genius and the fidelity of his execution ;
but it is in his pictures of the mountains of Sinai, Norway, and
ANNIVERSARY ADDRESS OF THE PRESIDENT. 49
the Alps that his excellence in rock-drawing of every kind is con-
spicuous. Overwork and anxiety first clouded and then terminated
a life which once seemed full of brilliant promise.
Dr. WitnEetM Purripe Scurmerer, Professor of Geology in the
Faculty of Sciences, Director of the Museum of Natural History,
and Professor in the University of Strasburg, a Corresponding Mem-
ber of the French Academy of Sciences and of the Academies of
Munich, Lisbon, and Philadelphia, elected a Foreign Correspon-
dent of the Geological Society in 1874, died of disease of the heart
on the 20th March, 1880.
Dr. Schimper was descended from a family living in the
Palatinate, the connexion of which with Alsace was at all times
close, and especially so during the first French empire. His
father at this time became the Protestant pastor of Dossenheim,
near Saverne, in Alsace; and here Schimper was born in 1808.
He was educated at first by his father, and from an early period
showed a great taste for natural history, which continued to
manifest itself after he had temporarily left the paternal roof, at
the age of 14, to pursue his studies at the College of Bouxwiller.
Here he remained until 1826, when he went to Strasburg, and
there, in 1833, took his degree as Bachelor of Divinity. He sub-
sequently acted for a time as curate ‘to his father, who was then
pastor at Offwiller.
_ he young Schimper, however, seems to have devoted his atten-
tion more to Natural History, especially Botany, than to theologi-
cal studies ; and he had acquired such a knowledge of the Mosses,
that as early as 1834 the eminent botanist Bruch proposed to
him that they should produce a joint monograph on the European
forms of that class of plants. Schimper acceded to the proposal,
and, with the view of devoting himself exclusively to natural-
history studies, resigned his ecclesiastical functions, not without
opposition on his father’s part, and in 1835 accepted the position
of preparator in the Museum of Natural History at Strasburg.
With that establishment he remained connected until the day of
his death, having been reinstated in his various offices by the Ger-
man authorities after their annexation of Alsace.
The work on European Mosses above mentioned was pro-
duced by Schimper alone. It is entitled ‘ Bryologia Huropzea, seu
genera Muscorum Huropeorum, Monographia illustrata,’ and is a
monument of the author’s industry and botanical attainments,
extending to six 4to volumes, with an atlas of 641 plates. Its
publication was commenced in 1836, but was not completed until
nearly twenty years afterwards (namely, in 1855). The author's
bryological publications did not cease then, however: he afterwards
produced several supplements to his great work, besides other
memoirs on Mosses, and a ‘Synopsis Muscorum Europeorum,’ of
which the second edition appeared in 1874.
In procuring materials for the above work, Schimper travelled a
good deal in various parts of Hurope; and on his journeys he was in-
50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
defatigable in collecting specimens of all kinds for the enrichment of
the museum under his charge. He acquired a very wide knowledge
of general natural history, and paid much attention to geological
phenomena, which, in conjunction with the direction of his special
botanical studies, early led him to the investigation of fossil plants,
upon which he was destined to become one of the chief authorities
of our day. He associated himself with Kochlin-Schlumberger in
the preparation of a great memoir upon the Terrain de Transition
des Vosges, published at Strasburg in 1862; to this Schimper con-
tributed the monograph of the fossil plants.
In 1849 he married a Swiss lady who had been long an ardent
student of botany, and who afterwards assisted him in his studies,
and especially in the accumulation of the vast stores of materials
upon which he founded his greatest work, the ‘ Traité de Paléon-
tologie Végétale,’ published in three large 8vo volumes, with a 4to
atlas of plates, of which the first volume appeared in 1869. This
important treatise upon the fossil flora will long be a standard
work of reference. Subsequently Schimper commenced the
botanical section of Prof. Zittel’s admirable ‘ Handbuch der Pali-
ontologie,’ which, however, he did not live to complete.
JosrpH Aveustin Husrerr Bosqunr, of Maestricht, Doctor of
Sciences, Pharmacien, Member of the Royal Academy of Sciences
of Amsterdam, was elected a foreign Correspondent of the Geological
Society in 1864. In 1868 the Council awarded the balance of the
proceeds of the Wollaston Donation Fund to Dr. Hubert Bosquet
as a reward for his valuable researches on the Tertiary and Cre-
taceous strata of Holland and Belgium. Dr. Bosquet worked out
with great industry and ability the fauna of the Maestricht beds,
a division of the Upper Chalk not present in England. His re-
searches amongst the Tongrian beds greatly extended our know-
ledge of these Tertiary deposits, both as regards their paleontology
and physical conditions. Bosquet’s labours were undertaken and
carried on amidst business duties, and with zeal and ability rarely
excelled. He was the author of twelve or fourteen contributions
both to geological and paleontological science. His chief papers
are :—‘¢ Description des Entomostracés fossiles de la craie de Mae-
stricht” (Mém. Soe. Sei. Liege, vol. vi. 1847); and “ Description
des Entomostracés fossiles des terrains tertiaires de la France
et de la Belgique” (Mém. Couronn. Bruxelles, xxiv. 1850-51).
His papers entitled “ Les Crustaecés fossiles du terrain Crétacé
du Limbourg” (Nederland. Geol. Kaart Verhand. 11. 1854) and
‘¢ Recherches Paléontologiques sur les terrains tertiaires du Lim-
bourg Néerlandais ” (Amsterdam, Verhand. vii. 1859), are of much
importance. Dr.Bosquet died on the 28th of June, 1880, aged
66 years and 10 months.
Prerre Henri Nyst, Conservator at the Museum of Natural
History at Brussels, was elected a Foreign Correspondent of
ANNIVERSARY ADDRESS OF THE PRESIDENT. 51
this Society in 1863, and in 1871 was elected a Foreign Member.
He was a Member of the Royal Academy of Sciences of Belgium,
and was also a Chevalier of the order of Leopold.
In 1874 the Council awarded him the balance of the proceeds ot
the Wollaston Donation Fund for his admirable, extensive, and
original researches upon the Crag Mollusca of Belgium. His chief
work is the ‘ Description des Coquilles et des Polypiers fossiles
des terrains tertiaires de la Belgique’ (4to, Brussels, 1843). Up
to the year 1873, Nyst had written about thirty-six papers, mostly
upon recent and fossil concholog ey. His connexion with the national
museum at Brussels, and obliging manner, rendered him at all times
accessible to students or those desiring information upon Tertiary
paleontology. Nyst died on April 6th, 1880, aged 67 years.
On tHe ANALYSIS AND DIsTRIBUTION OF THE British PALmozOIC
FossItzs.
Tux history of so progressive and practical a science as Geology,
and its kindred study Paleontology, especially during the past
decade, not only in Britain, but in Europe, America, and our Colo-
nies, now needs some revision and analysis, arising from the
amount of research, and the progress that has been made in these
and collateral sciences during this period.
The history of the Lower Paleozoic rocks of the British Islands
is almost the history of Geology; for it extends over forty years.
The same may be said of Scandinavia and Bohemia. And parallel
to these researches in Kurope may be recorded the great progress
made in the western hemisphere; for the history of the Lower
Paleozoic or oldest rocks of N. America and Canada is but that of
Britain and Northern Europe almost repeated ; homotaxially they
are the same.
The study through many years of the distribution of life through
the stratified rocks of the British Islands enables me to lay before
the Society some results arrived at by long and patient research.
I have, however, only taken advantage of my position on the
Geological Survey, which has afforded me facilities otherwise
almost impossible of access, and enabled me to carry on practically,
both in the field and the study, those branches of our science which
bear so intimately upon the progress of Physical Geology and Geo-
graphy, besides elucidating some of the laws that have governed
the distribution of life through time and space.
De la Beche, Lyell, Edward Forbes, Hamilton, Phillips, Huxley,
Ramsay, Prestwich, and Duncan, in their learned addresses delivered
from this chair, have one and all dealt with questions bearing
52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
especially upon stratigraphical geology as based upon the range and
distribution of organic remains, phenomena which since the time of
William Smith have been studiously kept in mind, teaching us the
succession of life and the relation in time of one formation to
another—each successive sedimentary group containing undoubted
records of its life and deposition, thus rendering clear and definite the
changes in, and the advance of life through time.
No more difficult problem exists cr remains to be solved than the
first appearance or commencement of life on the globe. Is the Lau-
rentian of North America, with its one known solitary form of life,
the oldest sedimentary rock existing? is Hozoon canadense the oldest
form of life? Research up to the present time has not revealed to us
one of higher antiquity ; neither has it even a truly associated form.
No true Annelide, Plant, or Protozoon accompanies this still mys-
terious progenitor of Paleozoic life.
The Hozoic or Laurentian gneiss of Britain or Europe, has not yet
yielded a semblance of any thing approaching Protozoic affinities,
although in the Hebrides, Norway, Sweden, Bohemia, and Bavaria
the Laurentian rocks have been recognized.
That the Laurentian rocks are not the oldest is manifest ; others
of infinitely greater age yielded sediment to the Laurentian sea,
and pabulum for the sustenance and material for the shelly structure
of its supposed only inhabitant ; but whether Hozoon had precursors
or not, time will probably tell.
Dr. Dawson, however, suggests that vegetable life preceded
Eozoon, and may thus have accumulated previous stores of organic
matter. If any older forms of animal life did exist, they cannot
have belonged to much simpler types; “naked Protozoa would
have left no sign of their existence, except probably minute traces
of carbonaceous matter.” Dr. Dawson in the year 1865 discussed
the question of associated organic structures, and what share, if
any, they may have had in the accumulation of the Laurentian
Limestone. Microscopic examination exhibited evidence of calca-
reous and carbonaceous fragments of organic origin. The contents
of the organic limestone, as shown by Dr. Dawson, were “‘ Remains
of Kozoon, other calcareous bodies probably organic, objects im-
bedded in the serpentine, carbonaceous matters, perforations or
worm-burrows.” Dr. Dawson strongly and fairly argues for asso-
ciated life.
The presence of graphite in large deposits occurring both in
beds and veins in the Laurentian rocks, clearly determines that its
origin and deposition were contemporaneous with the mass or con-
taining rock; the graphite, again, 1s associated with calcite, quartz,
and orthoclase. It is not improbable that the ‘ vein graphite ” was
introduced as a liquid hydrocarbon. Dr. Sterry Hunt believes it
possible that it may have been produced in a state of aqueous solu-
tion*. In the lower Laurentians the quantity is enormous. Dr.
Hunt also believes that the origin of the graphite was due to the
deoxidation of carbonic acid by living plants. That the graphitic
* Hunt, Report of the Geological Survey of Canada, 1866.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 53
matter of the Laurentian rocks was laid down or accumulated in
beds like coal is improbable, no evidence whatever tending to show
that there existed terrestrial vegetation. On the other hand, the
hydrocarbon may have been due to diffused bituminous matter
closely resembling “‘ our bituminous shales and bituminous and oil-
bearing limestones.” Research hitherto has failed to find traces of
any organism save the Hozoon ; no cryptogam has yet occurred ; and
we cannot imagine that, if of vegetable origin, the organic matter
could have been so completely disintegrated and bituminized prior
to being changed into graphite. Dr. 8. Hunt believes he has de-
termined the presence of terrestrial vegetation in the great beds of
Laurentian iron-ore which show subaerial decay, thus implying the
‘reducing and solvent action of substances produced in the decay
of plants.” Dr. Dawson long ago (1875) believed that he had found,
in the compact graphitic limestones of Clarendon, traces of fibrous
structure due to segregation which may be the remains of plants,
‘and in some specimens vermicular lines ” which he believed to be
“‘ Hozoon penetrated by matter once bituminous, but now in the
state of graphite.” At the utmost we can only speculate upon the
presence or condition of vegetation during the Archeean, or Pre-
Cambrian, Laurentian, or Eozoic time.
Dana employs the term Archzean in time, to express in full mean-
ing that era in the physical development of the Earth which was
‘“‘incompatible with the existence of life,” when life was not, so far as
we know. Little, however, is known of that vast group of rocks
we call Pre-Cambrian, adopting this term as used in this country,
on the Continent, and in America, for rocks affording us no history
or recognizable records.
Dana again assumes and endeavours to show that four eras pre-
ceded the Laurentian period :—
A first or molten era subsequent to that of the presumed original
nebulous state.
A second era, one of solidification and consolidation through
cooling, when the Earth became solid at the centre; later on, at-
mospheric vapours became condensed and probably universal ; water
covered all. The cooling and contracting of the sphere resulted in
oceanic depressions in special areas, and our continents were sha-
dowed forth and contoured, but as yet no life can be chronicled.
The third era may have given us surface reliefs; stratified deposits
were formed.
The fourth era probably saw the beginning of life, which occurred
when the oceanic waters may have stood at 200° F. With this
fourth era we may associate the Hozoonal serpentines.
In the British Islands we have yet to find that type of Laurentian
rock which yields either of the great limestones of Canada,—
the so-called Fundamental Gneiss of Scotland, Malvern, and Ire-
land having no affinities with the Eozoonal and graphitic group
of the North-American continent, and being doubtless of vastly
younger date.
To summarize the results of the labours and views of those who
VOL. XXXVII. ie
54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
have carefully investigated and thought out any great physical
question is at all times difficult ; and perhaps there are few subjects
on which men have theorized and differed more than on the history of
the globe. For time and life are two subjects that at once arrest the
attention of all earnest students. Our knowledge of the commence-
ment of either is as indefinite now as in the days of the earliest
investigators. With the succession of sedimentary rock-masses
in the outer framework of the globe we are perhaps partly familiar,
certainly so for given and known areas; there are, however, exten-
sive regions yet unknown and unexplored, and remaining to be corre-
lated with the known; and yearly in the Transactions of our Society,
through the researches of our Foreign Members and others, are we
reminded how insecure and uncertain is our base, how doubtful our
succession, when attempted to be universally applied. Yearly some
new light is thrown upon the obscure history of the earliest rocks with
which we believe ourselves acquainted. Both theearly metamorphic
and the lowest Paleozoic rocks, even in our own small area, are
still waiting for final position and classification; the same may be
said of much of Europe, America, Canada, India, and Australia.
Paleozoic time in Europe and Britain may have commenced with
the deposition of the so-called earliest Cambrian rocks; but where
geographically, we know not—probably far to the west of Ireland
and the British Islands, under what.is now the deep Atlantic. The
north-western coast of Scotland, and Ireland, much of the north-west
of England, and North and South Wales all point to a region where
we may believe that the earliest known sedimentary rocks of Western
Europe, and their life contents had their commencement or origin.
Little can be said here of Archean time and its rocks as developed
on the American continent; possibly we may recognize and correlate
the Archean system of Dana with our gneissose schists and so-called
Laurentian rocks of the north-west coast of Scotland and the
Hebrides.
It would be mere speculation here to attempt to define any strict
contemporaneity. We know from the labours of Dana, and the re-
searches of Sir William Logan in the field, and of Billings in the
study, that two periods or eras of Archean time are fully represented
in North America and Canada:—Ist, the older or Laurentian;
2nd, the Huronan, this latter in all probability represented by
our lowest Cambrian, or those beds underlying the Menevian of St.
David’s, and also constituting the rocks of Harlech, Llanberris, Ban-
gor, and the Longmynds. We have hitherto discovered no life-remains
in the Archean rocks of the British Islands, our so-called Lauren-
tians having none of the prevalent limestones, Eozoonal or otherwise,
of the New-York and Canadian rocks. To trace out the conditions
of the northern hemisphere during Lower-Cambrian times, both
zoologically and physically, has been and is still one of the most
difficult and important problems of modern geological research*.
We have long known that the. Huropean area was of great extent,
* Vide Hicks, Geol. Mag. dec. 2, vol. iii. p. 876, ‘‘ On the probable Conditions
under which the Paleozoic Rocks were deposited over the Northern Hemisphere. ’
ANNIVERSARY ADDRESS OF THE PRESIDENT. 55
even before the Cambrian rocks were accumulated : remnants of this
early land or continent are still visible and traceable in Spain,
France, Scandinavia, Ireland, Scotland, England, and Wales. Gneiss,
eranitoid rocks, and occasional limestones formed the mass of this:
Pre-Cambrian land, now exhibited to us in a greatly metamorphosed
state, stratigraphically unconformable to the overlying Cambrian,
and with a discordant strike north of latitude 380°. These rocks are
visible on both sides of the Atlantic as far as the Arctic regions,
representing portions of two continents, Hurope and America,
now separated by the North Atlantic.
Pre-Camprian Rocks.
it may be received as an axiom that all the known older sedi-
mentary rocks were deposited more or less in a similar manner,
or under similar conditions, to those of modern times. Allowing
this to be the case, it is most probable that those sedimentary
deposits which are the lowest, or have the earliest position, have
undergone most change; and it must be admitted that the erystal-
line, semicrystalline, and metamorphosed state in which they now
appear has been subsequently induced through various agencies
(beat, pressure, and chemical change) exerted through countless
ages. Research seems to prove that most of the rocks now recog-
nized as Pre-Cambrian were originally sedimentary strata, which
have undergone, since their deposition, alteration or metamorphism.
Few men have paid more attention to the physical history, distri-
bution, succession, and character of this most ancient group of rocks
than Dr. Hicks, ably followed by Professor Bonney, Professor Hughes,
Mr. Tawney, Dr. Sorby, Professor Hull, and Mr. Hudleston ; each of
these observers has contributed largely to the elucidation of the
history of the Cambrian rocks in his own particular way. Three
if not four groups or systems have been determined by Hicks, having
definite bearings or discordant strikes one to the other through
certain portions of the British Islands. They occur in ascending
order, and in the order of time, as follows :—
1. Lewisian. Hebrides and North-west Highlands.
2. Dimetian. St. David’s, Caernarvon, and Anglesey.
3, Arvonian. Pembrokeshire, Caernarvonshire, Anglesey, Shropshire,
and the Harlech Mountains.
4. Pebidian. South Wales, Shropshire, Charnwood Forest, Anglesey,
and Ireland.
Lrewistan.—Murchison gave the name Lewisian to the crystal-
line rocks largely entering into the structure of the Hebrides and
North-western Highlands; probably these constitute the oldest group
of rocks known or recognized in the British Islands. Red felspar,
hornblende, and quartz are the prevailing ingredients in these mas-
sive gneisses ; occasionally, as at Cape Wrath and on the coast to the
south, almost pure hornblende rock occurs. The strike of the
Lewisian group is usually east and west, or ranging between that
and north-west and south-east.
ee
56 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
The Malvern chain may also represent the Lewisian ; and also the
highlands of North Ireland as developed in Donegal.
Dimer1an*.—This group is extensively developed in many parts of
South and North Wales ; it oceurs in Shropshire, and, according to Dr.
Hicks, is known in the Worcester Beacon of the Malvern chain; it is
also said by Hicks to occur at Ben Fyn, Loch Maree, and near Gaer-
loch in Ross-shire, and in other areas in the N.W. Highlands.
Unlike the Lewisian type, the Dimetian contains impure chloritic
limestones and serpentinous bands (not of organic origin so far as we
know). ‘The chief minerals are flesh-coloured and white felspar, and
chloritic and hornblendic bands ; and the rocks are highly quartzose.
Fragments of the older Lewisian gneiss are occasionally found im-
bedded in the gneiss, thus determining the unconformability of the
Dimetian group, through derivation and denudation. Viridite occurs
more or less throughout, giving a tinge to the rock. At St. David’s
the ridge formed by these rocks, according to Dr. Hicks, averages from
2000 to 8000 feet in thickness. ‘‘ Cambrian conglomerates rest im-
mediately upon the Dimetian rocks ; and the highest members of the
Harlech group strike up against the Dimetian ridge;” and both
sides are flanked throughout by the uncomformable Pebidian group.
At St. David’s the rocks chiefly composing the Dimetian series are
compact crystalline quartz, chloritic schists, and indurated shales ;
the quartz in places occurs almost perfectly crystalline. Massive
beds of calcareous shale and dolomitic limestone occur. “ As muchas
20 per cent. of carbonates have been determined on analysis by
Mr. Hudleston, and in addition 0°5 per cent. of phosphoric acid ;
hence it is more than probable that the lime was deposited by
organic aid” (Hicks). The Pebidian rocks are strongly contrasted
by their bedded and shaly character. Dr. Hicks has not discovered
any traces of organic life in the inferior limestones, of which five
beds occur.
Dr. Hicks estimates the thickness of the St. David’s Dimetian at
15,000 feet. Several intrusive dykes traverse the series ; and their
injection took place before metamorphism had commenced. They are
fine-grained altered dolerites, columnar in structure, with the columns
at right angles to the plane of the dykes.
Arvontan.—In 1878 Dr. Hicks discovered in Pembrokeshire new
areas of Pre-Cambrian rocks of a totally different character from
the Dimetian and Pebidian which he had previously described.
The rocks of this Arvonian group are marked on the Geological
Survey map as intrusive felstones; they occur in three or four
isolated masses of considerable extent. Their strike is from north
to south, and discordant to those of the newer rocks and the under-
lying Dimetian.
The wild mountain-region of Plymstone is mainly composed of
the Arvonian group. Dr. Hicks finds Lower Cambrian and Lingula-
flag rocks resting unconformably upon the “ Arvonian” along their
* «Dimetia,” the ancient name for a kingdom which included this part of
Wales. Vide Hicks, “On the Pre-Cambrian (Dimetian and Pebidian) Rocks of
St. David’s,” Quart. Journ. Geol. Soc. vol. xxxiti. p. 229 (1877).
ANNIVERSARY ADDRESS OF THE PRESIDENT. 57
N.W. edge. The texture of this new group is hard and flinty,
some portions having an imperfect conchoidal fracture. The chicf
character or peculiarity consists in the manner in which the quartz
is separated or segregated into nests, giving the rock a pseudopor-
phyritic appearance.
The Arvonians, both generally and microscopically, closely re-
semble the Swedish ‘‘ Hilleflintas ;” nevertheless associated with
them are true quartz-felsites, probably old lava-flows (rhyolitic).
The evidence as to the position which the Arvonian occupies in the
Pre-Cambrian group is conclusive, as determined by the way in
which the Cambrian rocks are faulted down against it. It is cer-
tainly Pre-Pebidian, as fragments of the Hiilleflinta occur in the
overlying Pebidian conglomerates; its rocks occupy a large pro-
portion of the Dimetian axis of St. David’s; and, according to the
researches of Hicks, that part coloured as syenite and felstone in
the Geological map to the N.E. of St. David’s must be assigned to
the “‘ Arvonian” group, only the lower portion being Dimetian.
Like the Dimetian these rocks are greatly altered, consisting of
highly metamorphosed indurated porcellanitic shales. The beds
resting upon the Dimetian axis are hard compact conglomerates,
composed of quartz and altered shale derived from the Dimetian.
Prprp1an*.—The Pebidian rocks are unconformable to the Dime-
tian, extending along both sides of the Dimetian ridge. They
strike from §8.W. to N.E., nearly parallel to the ridge, or in
accordance with the overlying Cambrian Rocks; they are irregular
in thickness and greatly metamorphosed, composed of porcellanitic
shales; “the narrow dark lines” of stratification and closely
approximating and intersecting joints distinguish the Pebidians
from the Dimetian, against which they rest. ‘The “lower beds are
hard compact conglomerates, composed of masses of quartz and
altered shales,” derived from the underlying rocks and closely con-
nected together. ‘These all immediately lie on the Dimetian axis.
They are to be seen at Nun’s Well, south of St. David’s, on both
sides of the Caerbuddy valley to the east of the city, and north and
south of the cathedral in the valley. This Pebidian group supports
the true Cambrian rocks at many places in the neighbourhood.
Little more than 3000 feet are exposed; and the strike is nearly
identical with that of the overlying Cambrian. The large area
coloured as intrusive greenstone upon the Geological Survey map, and
extending parallel to Ramsey Sound, is composed of the Pebidians.
A considerable portion of the 8.W. part of Ramsey Island consists of
the compact porcellanites which characterize this series. The
Harlech conglomerates rest unconformably upon or along the N.K.
edge of the Pebidianst. Basic lavas and breccias predominate over
the Rhyolites.
It is stated by Professor Ramsay, in the ‘ Geology of North Wales’
* So named from ‘ Pebidiauc,” the name of the division or hundred where
these rocks are exposed near St. David’s. .
+ See Dr. Hicks, Quart. Journ. Geol. Soc. vol. xxxiii. pp. 229--239, for map
and sections &e.
55 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
(Mem. Geol. Surv. vol. iii. p. 8), that the oldest rocks in Wales and
Shropshire appear at the surface in six districts—elevation, denuda-
tion, and relative changes haying caused to be exposed as six inland
islands as many masses, chiefly mountainous, and composed of the
oldest sedimentary strata, in Britain, whose true history has yet
to be written. In Ireland we may recognize three or four such
areas also.
These and others, of the history of whose masses we are still
ignorant, constitute the basis and foundation (mostly unfossilife-
rops) of all succeeding sedimentary strata. They have been of late
and still are being subjected to critical examination, both chemically
and microscopically. Large areas hitherto believed to be of igneous
origin, and long ago mapped as such during the progress of the
Geological Survey, are now found under rigorous examination to
be sedimentary rocks which have undergone complete metamor-
phosis since deposition. Such determinations are all-important
when we come to consider the earliest appearance of life and its
distribution within the British area; for recent investigation has
resulted in the removal of certain rocks, hitherto believed to be
igneous, to the sedimentary or stratified series. This has been the
case, as we have seen, with several important masses in North and
South Wales, now designated Pre-Cambrian, assuming them to be
a group of rocks of higher antiquity than those in which undoubted
traces of life have hitherto been found in Britain.
To the influence of microscopic investigation and research is due
the right determination and history of these and other doubtful
rocks. Dr. Hicks has described some areas in the Lleyn peninsula
along the N.W. shore which he believes to be representative of his
Dimetian, Arvonian, and Pebidian groups; and Professor Bonney
doubts not, from microscopical examination, the presence here of a
considerable Pre-Cambrian series, with at least two very distinct
groups of rocks.
Dr. Hicks during the past summer determined the presence of
an older series of rocks than the Cambrian of the Harlech or
Merioneth anticlinal near the centre of the Harlech Dome. These
rocks evidently underlie the Harlech sandstones, and constitute
part of a pre-existing formation. The Cambrian conglomerates at the
base of the Harlech grits contain fragments of rock identical with
- this older formation.
No discovery of late has equalled this in importance ; it has proved
the existence in North Wales of a group or system hitherto un-
known, although expected or anticipated. This enables us to compare
the thickness of the Cambrian rocks of North Wales with that of
those of the same age at St. David’s in South Wales, and at the same
time to realize and compare the physical conditions of thetwo. This
may enable us to measure the thickness of the Harlech Cambrians,
and probably to arrive at the strike of the subjacent rocks. The
broken and denuded anticlinal has exposed these Pre-Cambrian
rocks, north and south ; they are marked in the maps of the Survey
as intrusive felstones, but appear to be a highly metamorphic
ANNIVERSARY ADDRESS OF THE PRESIDENT. 59
series of schists, alternating with bands of purplish slate, and
are believed by Dr. Hicks to be of Pebidian age: the strike is from
N.E. to S.W.
Between Caen Cochion and Pen-maen east of Traws-fynnyld road,
the Cambrian conglomerates are seen resting unconformably upon
the older series; and masses of the Pre-Cambrian occur plentifully
in the conglomerate. It is to be hoped that Dr. Hicks will continue
his researches over this wild and difficult region; it is highly im-
portant to know the precise nature of the axis and underlying rocks
of the anticlinal. The researches of Professor Ramsay and the
Survey detail all that we really know of the great mass of the
Harlech Dome or Merioneth anticlinal*. Caernaryonshire, Angle-
sey, Shropshire, the Malvern Hills, and Scotland have received critical
examination from Dr. Hicks; but his results are too full of detail to
be entered upon here.
The physical structure and life-history of the classical promon-
tory of St. David’s has of late years, at the hands of Salter and
Hicks, received an amount of research and attention of which
scarcely any other district can boast.
The rocks composing the ancient headland of Menapie are,
perhaps, the oldest known rocks containing organic remains in the
British Islands, if not in the world; nevertheless the characters
presented by the contained organisms are such that we cannot
imagine that we have here traces of the earliest manifestations of
life upon the earth.
In treating of the various successive formations embraced in the
recognized Paleozoic divisions of the British sedimentary rocks,
1 shall omit altogether any definite classification into great systems.
For while we may define one period as characterized by the
presénce of a certain fauna, which in the next succeeding so-
called epoch, is replaced by a different one, there will always be
found in some part of their geographical distribution a region
where, in some form or condition, the two faunas commingle,
and where the old one gradually disappears as the new one comes
in or makes its appearance. To assign, therefore, any definite or
precise boundary-lines or limitations to our stratified rocks and their
contents, when the record of past life is of necessity so incomplete
and obscure, is, to say the least, at present premature, if not unphi-
losophical, however convenient it may to a certain extent be; but
the progress of so boundless and progressive a science as Geology
with its associated subjects, demands that we should lay down no
hard or definite lines, no brackets or definitely constructed tables.
Each year witnesses the breaking-down of arbitrary divisional
lines in classification, in Zoology and Pale econtology as well as in
Geology. Any attempt, therefore, to establish geological divisions
or horizons upon either stratigraphical or paleontological breaks
must be temporary and local only; probably there exists no
break in life, any more than in time or in sedimentation; for some-
* Vide Ramsay, Mem. Geol. Survey of Great Britain, vol. iii. Geol. of North
Wales, pp. 17-19.
60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
where there will be found continuous and conformable succession
both physically and paleeontologically. We have no visible chrono-
logical scale in Geology but such as is afforded by the relative
magnitude of zoological changes; in other words, the geological
duration and importance of any system is in strict proportion to the
comparative magnitude and distinctness of its collective fauna.
It would be out of place here to enter upon the question which
has been long at issue as to the claims of two, if not three, schools
of thought and research in relation to the divisions or classification
of the Lower Palzeozoie rocks.
“¢ To Professor Sedgwick must be conceded the credit of determining
and assigning the limits and sequence of the larger subdivisions; for ~
single-handed he laid down with masterly precision the succession
and true stratigraphical arrangement of the Lower Paleozoic rocks
of Wales, from the Bangor beds to the summit of the Bala group.”
‘To Sir R. Murchison must also be awarded the high credit of
having been the first to distinctively assign to many of these rocks
their sequence, distinctive fossils, and palecontological value”*. Con-
flicting views led to the formation of a third school of research, in
which Sir Charles Lyell, Mr. Salter, and Dr. Hicks exercised great
influence. These last two observers assigned the term Silurian to
all the strata ranging from the top of the Ludlow to the base of the
Arenig, and restricted the term Cambrian to all between the base
of the Lower Arenig and the lowest known beds of the Harlech and
Llanberris group. The Tremadoc group, by its fossils, however, has
hittle in common with the underlying Lingula-flags and Menevians,
only sixteen of the Lingula-flag and other forms, out of one hundred
and eighty-two that range below the Tremadoc passing up to the
latter horizon. The great and almost total break at the top of the
Tremadoe lends strong evidence in favour of the division. being recog-
nized here.
The recognition of a tripartite grouping of the faunas and
strata, between the base of the Old Red Sandstone and the
Harlech series, cannot be disputed; each is characteristic, and
possesses a broadly-mark i ial Cam-
brian, or first fauna, the “Ordovician” system, or second fauna,
and the Silurian system, or third fauna, according to their succession
in time. Sedgwick named his system after, the entire principality
in which his rocks were typically developed, his. title of Cambrian
being comprehensive enough to embrace the whole of the Palecozoic
rocks. Murchison selected the term Silurian, associating the rocks
of his system with the tribe of the Silures.
Mr. C. Lapworth, in his able paper upon the tripartite division of
the Lower Palmozoic rocks, has suggested, and with good reason,
the name “Ordovician” for all that croup of strata in the Great
Bala district called Upper Cambrian of Sedgwick or Lower Silurian
of Murchison—from the ancient tribe of the Ordovices, who occupied
the country now called Montgomeryshire, Merionethshire, Caernar-
vonshire, Denbighshire, and Flintshire. So long, he remarks, as the
* Geol. Mag. decade 2, vol. vi. pp. 1-15, 1879.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 61
present system of nomenclature exists nothing can disturb the
application. of the title Cambrian to the rocks of the primordial series,
and of Silurian to the strata of the third fauna, or that series of
strata intervening between the Old Red Sandstone and the Lower
Llandovery. With the intermediate series from the Llandovery to the
Lower Arenig ‘‘ we have had incessant differences respecting nomen-
clature, proper limits of the groups, and sequence of fossils; they
are still designated as Upper Bala, Caradoc, Middle Cambrian, and
Lower Silurian. This central system of the Lower Paleozoic may
therefore well receive a name equally euphonious and significant of
the area where its strata are typically developed ” *.
No division of the British sedimentary rocks has given rise to so
much controversy as the so-called Cambrian strata. At the present
moment they have no fixed or definitely-assigned horizon, either
base or summit, beginning or end; their time-history, necessa-
rily their space-development also, rests upon no agreed or recog-
nized determination. ‘Two, if not three, schools of research in these
lowest groups of rocks differ even among themselves as to the
uppermost limit that should be assigned to the term Cambrian, or
where in the field the line of demarcation should be drawn between
it and the Silurian, or at the base between it and the Pre-Cambrian
or metamorphic series. It is no part of my duty to enter ito
details relative to the history of the controversy which has so long
occupied the minds and attention of the respective advocates of the
schools of Sedgwick and Murchison.
The past ten years have witnessed great changes both in the
nomenclature and classification of the Cambrian rocks. The name
Cambrian, given by Sedgwick in 1838 to the whole group of strata
below the May-Hill Sandstone, has of late years again given rise
to much controversy. This critical research has been equally
important in its bearing upon the investigation of European and
American geology and the establishment of a corresponding no-
menclature for the succession and history of these oldest known
fossiliferous rocks on the globe. Whether we can rightly refer
the Dimetian, Arvonian, and Pebidian groups of Britain to the
Laurentian and Huronian of Canada is yet a question; that they
occur below the recognized Cambrian, there can be no doubt, both
from discordancy of strike, petrological differences, and supposed
total absence of organic remains. Probably the great groups of rocks
comprised under the above names (Laurentian and Huronian), the
Archean of Dana, may be the equivalents in time of our St.-David’s
and North-Wales Pre-Cambrian; and his Primordial or Cambrian
system (embracing the two series Acadian and Potsdam) may repre-
sent the lower portion of our fossiliferous Cambrian rocks, or those
so well defined and developed at St. David’s, viz. the red shales and
flaggy beds. with Lingulella ferruginea and L. primeva, the red,
purple, and grey grits, the Plutonta-beds, the red, grey, and purple
flagey sandstones, and the succeeding grey flaggy series, all five of
which are fossiliferous. Not only so, but these Pembrokeshire Cam-
* Loc. cit. p. 14.
62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
brian rocks seem to have no equivalents in North Wales, unless they
represent in time the Llanberris, Harlech, and Bangor sandstones,
grits, and flags, which, however, have as yet yielded no trace of organic
remains. Again, very few species are common to these grey, red, and
purple sandstones and the succeeding well-developed Menevian
group, which has yielded nearly fifty species* ; yet in the Harlech,
Barmouth, and Dolgelly areas the Menevians immediately succeed,
are conformable to the underlying barren unfossiliferous grits, and
exhibit the first traces in North Wales of a definite and defi-
nable fauna. In other words, the representatives of the Harlech
and Llanberris beds in the St.-David’s promontory contain a
well-marked fauna, highly characterized by the Crustacea (7
genera and 14 species) and by the still more important fact
that no species occurring in the Longmynd and Harlech rocks of
St. David’s are known in North Wales. It is only in the succeeding
Menevian (Lowest Lingula-flags) that there is a well-marked com-
munity. Of the 12 Pembrokeshire species (9 of which are
Trilobita, viz. Agnostus cambrensis, Conocoryphe bufo, C. Lyellir,
C. solvensis, Microdiscus sculptus, Paradowides aurora, P. Hicksw,
P, Harkness, and Plutonia Sedgwickit) not one is known out of
the area; whereas of the 28 Menevian species known in the St.-
David’s area, 12 are common to it and North Wales and 5 are con-
fined to North Wales, viz. Agnostus reticulatus, Ang., Anopolenus
ampar, Hicks, Conocoryphe coronata, Barr., C. Homfrayi, Salt.,
and Hrinnys venulosa, Salt.; 7 are common to both areas, and
16 peculiar to the Menevian promontory. These will be referred
to under the Menevian group.
This non-occurrence of fossil remains other than Annelide-burrows
(Chondrites and Cruziana) in the Cambrian of the Geological Sur-
vey has much significance when they are compared with groups of
rocks equivalent in time, and not far removed geographically, meta-
morphism not haying affected their original condition so as to have
obliterated all traces of life. The sequence in both areas (North and
South Wales) is the same, as proved or determined by the position
of the Menevian beds, which in South Wales have a fossiliferous
base in grey, red, and purple sandstones, these, again, resting upon
a Pre-Cambrian foundation of highly metamorphosed rocks, divisible
into three systems or formations, which Dr. Hicks has denominated
Dimetian, Arvonian, and Pebidian, all having different strikes or
bearings. We must remember that the Menevian beds of North
Wales rest (so far as is at present known) on the unfossiliferous
Bangor, Llanberris, and Harlech grits throughout their known ap-
pearance and range.
Lower CAmBRIAN Rocks.
The fossils which occur in the lowest known part of the Harlech
and Bangor group at St. David’s are Lingulella ferruginea, Salt., L.
* The Middle Cambrian or Lower Lingula-flags of Sedgwick, the Lingula-
flags of authors, and the Upper Cambrian of Lyell and Salter; the Menevian
group of Salter and Hicks.
. ANNIVERSARY ADDRESS OF THE PRESIDENT. 63
primeva, Hicks, Discina, sp., D. caerfaiensis, Hicks, and Leperditia
cambrensis, Toles: these all occur in the lowest red shales below the
sands at Castell, on the east side of Ramsey Sound. About 1000 feet
of unfossiliferous red and purple grits and sandstones succeed this
first known fossiliferous group; then, in yellowish-grey flagg
sandstones, between Porth-Clais Harbour and Caerbuddy, we meet,
for the first time, with the gigantic Crustacea (Trilobita) Plutonia
and Paradowides, and associated with them two genera, Microdiscus
and Agnostus, almost microscopic in size, and at the same time, or
in the same beds, Protozoa belonging to two species of Hexacti-
nellid sponges, Pr otospongra fenestr ata, Salt., and P. major, Hicks,
and also two species of Pteropoda, Theea antigua, Hicks, and ..
penultima, Salt. I particularly mention this first assemblage of
life, as being, so far as I know, the earliest in the earth’s aston "y
on record; and it consists nevertheless of forms whose organiza-
tion was not embryonic; thus distinctly pointing to a line of an-
cestors belonging to this or some other area yet to be determined.
The entire fauna of these Plutonia-beds consists of 8 genera and
9 species, 5 of which are Trilobita (viz. Plutonia Sequickii, Hicks,
Paradoxides Harknessii, Hicks, Oonocoryphe Lydellii, Hicks, Micro-
cascus sculptus, Hicks, ’ Agnostus cambrensis, Hicks), two Protozoa
(Protosponyia fenestrata, Salt., and P. major, Ticks), with Lingulella
ferruginea, Salt., and Theea antiqua, Hicks; three of these, Para-
dowides Harknessri, Agnostus cambrensis, and Protospongia fenestrata,
pass to the Menevian group. Plutoma Sedgwicku, Conocoryphe
Lyellia, and Microdiscus sculptus have not been detected in any
higher horizon, and P. Harknessii only in the succeeding red,
grey, and purple flagey sandstones, where it is associated with
Conocoryphe solvensis, which represents Conocoryphe Lyellic below.
Grey and purple sandstones, 1500 feet thick, but with a scanty
fauna of only five species, including the doubtful Hophyton, succeed
the Plutonia-sandstones. Finally the Harlech and Llanbezris group
at St. David’s terminates with grey flaggy sandstones, which contain
another form of Paradoxides (P. aurora), Conocoryphe bufo, Hicks,
and Agnostus cambrensis, Hicks; in all eight species are known to
occur.
This first incoming of life in the British rocks and in the St.-
David’s area exhibits a singular assemblage and grouping of
species, doubtless owing to our limited acquaintance with’ the then
existing fauna, rendered obscure through the present state of our
collections. Numerically the fauna of the Lower Cambrian com-
prises 61 genera and 182 species, ranging from the lowest red
shales of the Longmynd group to the top of the Tremadoc. The
Longmynd and Harlech beds yield 18 genera and 32 species, the
Menevian group of South Wales 24 genera and 51 species, the
Lower Lingula-flags of all localities 17 genera and 36 species, the
Upper Lingula-flags 14 genera and 41 species, the Lower Tremadoc
29 genera and 59 species, and the Upper Tremadoc 20 genera and
33 species. Of this Lower-Cambrian fauna (61 genera and 182
species) only 9 genera and 12 species pass to the Arenig; of these,
64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
5 are Trilobita (Asaphus affims, M‘Coy, A. Homfrayz, Salt., Chewrurus
Frederici, Salt., Dionede atra, Salt., and Ogyqua scutatria, Salt.). It
will be observed that these are all Tremadoc species, none of the earlier
or more pronounced Longmynd, Menevian, and Lingula-flag forms
ever appearing above the Lingula-flags; but assuming that the
Tremadoe rocks terminate the lower division of the Cambrian series,
they must be acknowledged to be of value.
The species of Brachiopoda, as we should expect, tell much the
same tale. They are Lingulella pruncva, L. ferruginea, var. ovalis,
and Obolella maculata, which do not pass out of the lowest divi-
sions; while Lingula petalon, L. lepis, Lingulella Davis, Obolella
plicata, and Orthis Carausi, O. lenticularis, and O. menapice unite
the Tremadoc to the Arenig. The remaining species are pelagic
Mollusca. No Gasteropoda occur, and no form of Lamellibranch until
we reach the Lower Tremadoc, where 12 species are met with, thus
showing this earliest known fauna to have been highly specialized
and of long duration ; this would be expected from the great physical
development of the rocks, as well as through the large crustacean
fauna, which numbers 28 genera and 108 species, only 5 of which
passed to the succeeding horizon, or the Arenig, as before stated ;
none of the great Olenide (Paradowides, Plutonia, and Neseuretus)
passes to the higher division of the Cambrian or Cambro-Silurian
rocks.
The Pelagic fauna, 5 genera and 18 species, as exemplified by the
Pteropoda and Heteropoda, was, and is still, the largest known, in-
cluding Cyrtotheca 1 species, Theca 14, Stenorenn 1, Conularia 1,
and Beller ‘“ophon 1. Nine of these are St.-David’s forms ; and only
2 species of Pteropoda, Theca simplex and Conularia Homfrayi,
with Bellerophon multistriatus, pass to the Arenig ; they will also be
noticed under that group.
Pranra.—Granting that the Oldhamiw might be caleiphites, or cal-
careous corallines, resembling i in habit the Melobesice and Nullipore
of modern seas, or the group of corallines so abundant in the seas
of warmer latitudes, we are still at a loss as to their true nature,
even if organic at all. Gdppert refers them to sea-weeds, and com-
pares O. antigua with the living /zagora ramellosa of Kiutzing
from Teneriffe ; but Goppert makes two genera of Oldhania; Mur-
chisonites and Oldhamia, the O. antigua of Forbes being his Mur-
chisonites antiqua. Professor Kinahan and Edward Forbes both
referred. them to the class Hydrozoa as having affinities with the
Sertulariide*. The Rev. Mr. Berkeley long ago suggested a resem-
blance to the genus Acetabularia, one of the Ghiarospenmes (Chloro-
sporex). No traces whatever of these singular remains have been
found in any of the Cambrian rocks, either in North or South Wales.
Mr. Salter well searched the Cambrian erits near Bangor and Harlech
for Oldhanie ; but nothing approaching them was ever detected.
Probably their place, in the absence of better evidence, is amongst
the Hydrozoa. It is singular that, amidst these grandly developed
* Vide Baily, ‘Figures of Characteristic Brit. Foss.’ vol. i. Paleozoic, p. 1,
t. | (1875). ‘This book should be in the possession of all students of Palxozoic
paleontology.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 65
rocks of Wales, both North and South, no traces of this doubtful
body have occurred. |
Prorozoa.—Four species of Hexactinellid sponges (by no means
uncommon in the Longmynd and Menevian rocks of St. David’s)
have been described. ‘Three of the four species belong to the Har-
lech beds, below the Menevian; and all four occur in the Menevian.
Protospongia fenestrata, Salt., is also from the Lower Lingula-flags
proper. Zittel places these sponges in the family Euretide with the
Hexactinellide, and in the group Dictyonina. Mr. Carter believes
them to be the remains of sarco-hexactinellid sponges, which Mr.
Sollas has confirmed*. Mr. Salter was the first to notice these Amor-
phozoa in the lowest and oldest rocks of Wales. ‘The original form of
these sponges we know not; it may have been fiat and incrusting,
like Grantia. Mr. Sollas suggests that they may have been “ sacci-
form ” and anchored in the slimy ooze of the sea-bottom by a tuft of
anchoring-spicules?. The spicules were originally siliceous, but are
now converted into iron pyrites. The fact also that the spicules are
separate, not being “ enveloped in a common coating, or united by
ankylosis, clearly places or assigns them to the group Lyssakina of
Zittel, nearly equivalent to Carter’s division of the Sarco-hexacti-
nellide.” The species known are Protospongia diffusa, Salt., P. fene-
strata, Salt., P. major, Hicks, and P. flabellata, Hicks. No traces
of these have occurred either in the Harlech, Longmynd, Menevian,
or Lingula-flags of North Wales. They may be sought for round
the Harlech Dome, amidst the black shales and flags of the Menevian
beds.
AwnetipA.—The Longmynd group yields four genera and five
species, Arenicolites uricomiensis, Call., A. sparsus, Salt., Scolrtes
socialis?, Haughtoma pecila, Kin., and Histioderma hibernica, Kin.
If the quartzites of the Wrekin in Shropshire are of the age assigned
to them by Dr. Calloway, then the Arenicohtes uricomiensis of that
author is, with the exception of Hozoon canadense, the oldest known
fossil. Beyond the doubtful Annelidan tracks, and one species (Are-
nicolites sparsus) from the Longmynd group of England and Wales,
we have no determined species. ‘l'wo of the five species (Haughtona
pecla, Kin.) and Histioderma hibernica, Kin., are Irish, from near
Bray Point. Nine out of ten of the so-called fucoidal or plant-
remains in the rocks below the Devonian are only Annelide-burrows.
CrustAcEA.—Seven genera and 14 species occur in the lowest
Cambrian or Harlech rocks of St. Davids, 10 of which are confined
to them; the remaining + species (Agnostus cambrensis, Conoco-
ryphe bufo, Paradoxides aurora, and P. Hicksw) connect the Har-
lech and Longmynd Crustacea with the Menevian. The 7 genera
are <Agnostus, Conocoryphe, Leperditia, Microdiscus, Paradoxides,
Plutoma, and Paleopyge: 2 species of Conocoryphe (C. Lyell and
* See Quart. Journ. Geol. Soc. vol. xxxvi. pp. 362-367, Sollas “On the
Structure and Affinities of the Genus Profospongia.”
t+ This has been confirmed through the occurrence of another form in the
same family, lately described by Mr. Sollas from the Silurian of Canada.
66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
C. solvensis), 3 species of Leperditia (L. ferruginea, L. cambrensis,
and L. primceva), Microdiscus sculptus, and Plutonia Sedgwicki
are all confined to the Harlech and Llanberris group of St.
David’s. They constitute the Crustacean fauna of that horizon,
out of 103 species known in the six divisions of the Lower Cam-
brian rocks, and up to the close of the Upper Tremadoc. The Me-
neylan group possesses the largest Crustacean fauna in the eleyen
classes, and, except the Brachiopoda, the largest number indi-
vidually.
Hyprozoa.—No form known below the Upper Lingula-flags or
the Lower Tremadoc, from which Dr. Callaway has obtained the
earliest known species, Bryograptus Callavei, Lapw. Mr. Lap-
worth’s genus occurs in the Shineton shales of Shropshire. The
same genus occurs in the Olenus-beds of Westrogothia, in Sweden,
Linnarsson having detected these oldest Rhabdophora in that area.
Bracutopopa.—Only 6 species are essentially Lower-Cambrian
or Harlech forms, Discina pileolus, D. caerfaiensis, Lingulella ferru-
ginea and var. ovalis, L. primeva, and Orthis sagitialis; this last
species is doubtful. Five genera and 20 species range through the
six horizons, or from the Longmynd group to the Upper Tremadoce ;
but, as we have seen, only the 6 just named occur in the lowest
horizon ; 4 of these belong to the Tretenterata (non-articulate group).
It is doubtful if the others occur in the Longmynd group.
LAMELLIBRANCHIATA.—No bivalve mollusk is known to occur
below the Lower Tremadoc. In that formation for the first time
in Britain we recognize 5 genera with 12 species. Davidia and
Glyptarca are new ; the remaining 3 are the well-known genera
Modvolopsis, Palearea, and Ctenodonta. This may be regarded as the
first well-determined appearance of the Pelecypoda in any region.
GastEropops.—None known in the whole of the series of forma-
tions below the Arenig, where four genera seem to be recognized,
both in South Wales (St. David’s) and in the Stiper-stones area.
Pleurotomaria Uanvirnensis, Hicks, Huomphalus corndensis, Sow.,
and forms of Ophileta and Rhaphistoma occur.
Prpropops.—The six horizons of the Lower Cambrian yield 4
genera, Cyrtotheca, Stenotheca, Theca, and Conularia, and are repre-
sented through the six divisions by 11 species; but only 2 occur in
the Longmynd group of St. David’s under analysis (Theca antiqua,
Hicks, and 7’. penultima, Salt.). The Menevian beds of the same
area have yielded 6 species, to be noted under that group of rocks,
and the Lower and Upper Tremadoc 9 species. During the Arenig
and Caradoc periods only, have we to record so many pelagic Mol-
lusca; 8 species occur in the Arenig, and 10 in the Caradoc.
Hursroropa.— Bellerophon is the only form that occurs in these
lowest rocks; but no species has been recorded lower than the so-
called Middle Lingula-flags, where, as B. cambrensis, Belt, the genus
first BU Nee, associated with Hymenocaris vermicauda and Cono-
coryphe in the Upper Ffestiniog rocks ; but four of the five known
species are Tremadoc, where, specifically, the genus becomes of im-
ANNIVERSARY ADDRESS OF THE PRESIDENT. 67
portance. B. nultistriatus, Salt. (an Upper-Tremadoe species), unites
the Heteropoda of the Lower with those of the Arenig or Middle
Cambrian group.
CrrHaLopopaA.—No form or species known until we reach the
horizon of the Tremadoc rocks, where for the first time we find
both Cyrtoceras and Orthoceras, one species of each genus. Cyrto-
ceras precox, Salt., is, I believe, the earliest Cephalopod known. The
Lower Tremadoc rocks of Llanerch, west of Portmadoc, yielded the
Cyrtoceras ; and the Upper Tremadoc of Garth, and Llanvirn, St.
David’s, O. sericeum. The latter passes to the Arenig rocks.
We have thus seen how unequally distributed (as we should ex-
pect) are the zoological groups through the lowest Cambrian rocks,
and how distinctively certain genera characterize them, and, as will
be found upon a separate analysis of the Menevian, Lingula-flags,
and Tremadoc beds, how distinct a period is represented by all below
and up to the close of the Tremadoc age. The six divisions of the
Lower Cambrian represent the earliest history of the British rocks ;
for out of the 61 genera and 182 species known to range through
them, only 11 genera and 16 species pass to the Arenig or base
of the Lower Silurian, or Middle Cambrian (see Table VII.).
Taste 1.—Longmynd, Harlech, and Llanberris.
Classes. Genera. | Species. ne oe |
LPTe ance ave te ee eS Qin are
PAROLOZOM raise secs tele Sesotecs 1 3 x
Hydrozoa.
Actinozoa.
Kehinodermata.
Ja CILIC ERS UR Ce MRR ees 4 | 4.
Wisistaccan cee ee seen sce: i 14 z
Bryozoa. |
Brachiopoda ...............+.- 3 6 a
Lamellibranchiata.
Gasteropoda.
HREEROWOOAL. tlie. cisecsccavosc 1 2 i
Heteropoda.
Cephalopoda.
18 32 Be
Dr. Hicks has favoured me with a new classification for the
Lower Cambrian (Longmynd and Harlech) rocks of St. David’s:
the geographical significance of the names employed renders them
of value; and nothing of the kind has been previously attempted
below the Menevian group :—
68 PROCHEDINGS OF THE GHOLOGICAL SOCIETY.
( Up bee Sandstones and shales, with Orthis Hicksii &e.
VOOR:
op hel at
ee re e \ Flags and slates, with Paradoxides Davidis.
al i
{ ae \ Grey flags, with Paradoxides Hicksit &c.
( ca oa Grey rocks, with Paradowides aurora &e.
| Grey, purple, and red rocks, with Paradowxides solvensis
group.) 1500 ft. | (Hicks, MS.), Conocoryphe solvensis, &c., also Hophy-
{
Solva 4 Middle,
i __ ton and large fucoids.
| Lower, { Yellowish grits, sandstones, and flags, with Paradoxides
| 150 ft. | Harknessii, Plutonia Sedqwickit, &c., also Eophyton.
( Upper, \ Purple sandstones, with Annelids.
1000 ft.
ee | se Red shales and schists, with Leperditia cambrensis,
OEE Middle, Lingulella primeva, Discina caerfaiensis (Hicks,
group. | 50 fi. | MS), &
|
Lower, { Conglomerates and green flaggy sandstones, with An-
520 ft. | nelids.
Below the Caerfai group in South Wales, at St. David’s, occur the
Dimetian and Pebidian rocks, Pre-Cambrian in age, unconformable
in position, and discordant in strike ; they constitute the well-defined
axis of the St.-David’s promontory. |
MENEVIAN*® AND LINGULA-FLAGS.
In 1865 Messrs, Salter and Hicks gave the name to and established
this group of strata in the St.-David’s promontory, Pembrokeshire rf ;
it constitutes the lowest division of the Middle Cambrian of Sedg-
wick, and equals his Lower Lingula-flags, and is embraced in the
Lingula-flags of authors and the Upper Cambrian of Lyell and Salter ;
it is also recognized as being equivalent to Barrande’s Ktage C in
Bohemia ; it occurs in Sweden, has been recognized in North Ame-
rica and Canada, and is the St.-John’s group in Newfoundland.
The Menevian is now recognized as a separate division or sub-
group, distinguished from the Lingula-flags proper above, as the
Ffestiniog of Sedgwick was applied to the Middle and Upper groups
of the Lingula-flags in North Wales. In South Wales the Menevian
is about 700 feet thick, and more or less fossiliferous throughout.
Probably the base of the Menevian cannot be separated from the
underlying grits and sandstones of the Harlech and Bangor series,
passing as they insensibly do into them, both in North and South
Wales, and also into the true Lingula-flags above. No fossils occur
or have yet been detected in the grits and sandstones of the imme-
diately underlying Harlech rocks, which comprise the structure
of the Harlech Dome (Merioncthshire anticlinal of Sedgwick); the
same may be said of the great and exposed masses of these Lower
Cambrian rocks of the Bangor area, obscure traces of Annelide-
* Meneevia is the classic name for St. David’s. ; y
+ First announced at the British Association, Birmingham, 1865, ‘ Report,
p. 281.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 69
tracks (Chondrites) and burrows (Arenicolites) being all that has re-
warded patient research ; but below the primordial Menevian, as
we have seen, in the promontory of St. David’s, there exist greenish,
grey, and red flaggy or shaly sandstones, with species of Lingulella
differing from the typical LZ. Daviswz of succeeding age. In the
yellow, grey, and purple sandstones and flags we have the first
known Trilobites; and these are of gigantic size—the two genera
Plutona and Paradoaides, with Conocoryphe, demanding from us
the belief that they were by no means the first of Cambria’s Crus-
tacea.
The earlier highly metamorphosed rocks below the Caerfai group
and the Plutonia-sandstones in all probability contained the pro-
genitors of these early giants ; nowhere else in the British islands,
Kurope, or America have species been found of such high antiquity.
To the untiring energy of Dr. Hicks we owe the discovery of these
rocks and the description of the species contained in them.
The Menevian of the §$t.-David’s area rests upon and passes
insensibly down into the fossiliferous Harlech and Bangor rocks,
which contain an earlier fauna, which is not at all represented in
North Wales, either at Harlech or Bangor. Only one of the five
species of the great Paradoaides found in the pre-Menevian and
Menevian beds of South Wales is known in North Wales. The
long-known and solitary specimen called P. Forchhammeri, from
an unknown locality, is now determined to be P. Hicksii, which
occurs sparingly in the Menevian beds on the Camlan river north
of Dolgelly, but more abundantly with its two congeners, P. aurora
and P. Davidis, in South Wales, the fourth species, P.’ Harknessii,
characterizing only the Harlech group at St. David’s*. Associated
with these large Menevian Paradowxides, other forms, equally sig-
nificant, occur, viz. Holocephalina inflata, Hicks, H. primordialis,
Salt., and Carausia menevensis, Hicks; and they range no higher,
being distinctively typical or characteristic species of this horizon.
Two species of Anopolenus (A. Henrici, Salt., and A. impar, Hicks)
are common to the two areas, the former occurring at Rhaidr-ddu
valley, Tyddyngwladis, near Dolgelly, the latter at the Maentwrog
Waterfall.
No less than 6 species of the genus Conocoryphe occur in the
Menevian group: 3 characterize the St.-David’s, and 2 the North-
Wales beds; and 1 species, C. applanata, is common to both
areas. Conocoryphe humerosa, Salt., C. bufo, Hicks, C. solvensis, St.
Davyid’s only ; C. coronata, Barr., C. Homfrayi, Salt., North Wales,
Maentwrog; C. applanaia uniting the two areas. Hrinnys venu-
losa, Salt., and Arionellus longicephalus, Hicks, are both found in
the Waterfall-valley at Maentwrog, and the latter also at St. David's.
I draw attention to this group of Crustacea because they are strati-
graphically important, and constitute by far the most characteristic
* Dr. Hicks has added another species from the Trelewr beds below the
Menevian, P. solvensis, associated with Conocoryphe solvensis and the so-called
Eophyton.
VOL. XX XVII. g
7O PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
portion of the fauna of the lowest Cambrian rocks. No less than
9 genera and 26 species occur in the Menevian rocks alone of North
and South Wales; or, in other words, more than half the known
fauna is Trilobitic. In the Menevian beds occur the first known
Cystidean, a few fragments having been found by Dr. Hicks, in 1872,
associated with Pteropoda (Theca) and Entomostraca. The finding of
Paradoaides Davidis and P. Hicksvi at Dolgelly, on the same horizon
as that of St. David’s, immediately above the “‘ Cambrian” sandstones
(Harlech and Barmouth beds), in bands of uncleaved Menevian slate
and ashes, aids greatly in the correlation of the two areas. This, with
other evidence, justified Hicks and Salter in regarding the Menevian
and the Lower Lingula-flags as a well-marked division or subgroup
differing from the Upper Lingula-flags, quite as much so as do the
Upper Lingula-flags from the overlying Lower Tremadoc slates (as
now understood) ; for, with few exceptions, the species in each are
peculiar, and they possess many peculiar genera. I may mention
the following as genera that first appear in the Menevian beds; and
those marked with an * are confined to that horizon :—
Cystideas 2 see . &Protocystites.
Amelia eee eee .. xArenicolttes.
Crusticcas eee x Arionellus.
Bee Un rprt ah bie ene + Anopolenus.
Pa ate aaa ne eid OS * Hronnys.
BENE ANU ee * Holocephalina.
* Carausia.
AOA neers Hare Primitia.
Br achiopoda PNT eee ? Orthis
net ee Obolella.
Pteropoda SN asatet cae aes x Oyrtotheca.
MAUR we ietisn ac, Ry x Stenotheci. j
Although four oe of Protozoa (Protospongia. ee Salt.,
P. fenestrata, Salt., P. major, Hicks, and P. flabellata, Hicks)
occur at St. David's, the three first named species commenced in
the Harlech beds ielow, P. fiabellata being Menevian only.
No Protozoa have yet been detected in the North-Wales area.
Prior also to the year 1863 we had no knowledge of the exist-
ence of the gigantic Olen, revealed to us by the researches of
Salter, who disentombed the great Paradowides (P. Davidis) from
the black slates of Porth-y-rhaw and Solva Harbour, thus showing
the occurrence side by side in the same beds of the largest
Trilobite known with Agnostus the smallest. Both these genera
are remarkable ; and their extremes widely depart from the general
type. meas
Mh valuable paper was communicated to our Society in 1867,
vol. xxiii., by Prof. Harkness and Dr. Hicks, “On the Ancient Rocks
of St. David’s Promontory, South Wales, and their Fossil Contents.”
The authors dealt fully with both the seology and the paleontology
of that remarkable promontory. The chief portion of the labour and
ANNIVERSARY ADDRESS OF THE PRESIDENT, rie
research, however, was due to Dr. Hicks, whose intimate acquaint-
ance with the area and knowledge of the fauna of the Cambrian
and Silurian rocks enabled him to add largely to the palzontology
of the district. The authors described the great series of red, purple,
green, and grey rocks below the fossiliferous grey Menevian beds.
The history of these variously coloured sandstones, as revealed by
the researches already made in them, has an important bearing
upon our knowledge of the distribution of life through the Cambrian
and Silurian series of North Wales, with which they must be
correlated, the St.-David’s series yielding a fauna not yet known
in Monmouthshire, Caernarvonshire, or Montgomeryshire, or beneath
the Menevian and Lingula-flags of North Wales, which contain
organic remains older than, and different in species from any hitherto
discovered in Britam. The underlying Cambrians repose upon a
conglomerate, composed of quartz and other pebbles cemented in a
purple or red arenaceous matrix, which occurs on both sides of the
so-called Pre-Cambrian ridge or axis. That this quartziferous,
metamorphosed, crystalline, and unconformable mass underlies and
is older than the whole series of the Lower Cambrian rocks of that
area is certain; and, as such, it is the key to the physical structure
of the ancient headland of St. David’s. Subsequent research by
Hicks has determined that this extensive and exposed Pre-Cambrian
area is composed of three distinct groups of metamorphosed sedi-
mentary rocks of different ages, and having different or discordant
bearings or strikes*. Higher still, and also unconformably, succeed
the rocks of the Harlech or Longmynd group, which lie both to the
east and west. Until the Longmynd, Harlech, and Meneyian fauna
was discovered and worked out at St. David’s, and the last named
subsequently developed in North Wales, the lowest sedimentary
rocks of Britain then known were believed to be almost devoid of
life or “‘ barren in fossils.” Now, however, a remarkable fauna has
rewarded the researches of many distinguished labourers, and the
two areas have been carefully compared and correlated. Consider-
able differences exist, of which the causes are as yet unknown;
much has yet to be done in the paleontology of both these classical
districts. The non-discovery or absence of the genus Olenus in the
Menevian and Lingula-flags or primordial rocks of St. David’s is
singular, and at present inexplicable. The genus is abundantly
represented in both the Lower and Upper Lingula-flags of North
Wales, where no less than 12 species are known, 4 in the lower
division and 8 in the upper; and 4 distinct forms (viz. O. bisuleatus,
O. scarabeeoides, O. humilis, and O. pauper) occur in the Upper Lin-
gula-flags of Malvern, overlying the Hollybush sandstones. The
species O. scarabeoides (O. spinulosus, Phill.) is found also in the
Upper Lingula-flags of Carreg-Wen, west of Portmadoc.
Comparison of the earliest known faunas in Hurope and America
with that of St. David’s shows conclusively that they are identical as
to age or time of deposition and in genera also. This Angelin has
* See p. 56 ef seq.
g2
12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
demonstrated through his researches into the alum shale of Sweden ;
and the primordial fauna of Barrande has yielded Paradowxides, Cono-
coryphe, Agnostus, and Ellipsocephalus, the first three of which are
characteristic British genera.
Sweden has afforded P. Hicksw and other forms like our own.
The Spanish primordial rocks yield genera identical with those of
our Menevian and Lingula-flags—Puaradowides, Conocoryphe, Ario-
nellus, and Agnostus. America, has its Acadian group, with Para-
doxides &c. The Protozoic schists of Bohemia (Region C, Barrande),
also contain Paradoaides (P. bohemicus), Sao, Conocoryphe, and
Agnostus. The same conditions prevail in Canada and New Bruns-
wick. It would thus appear that all the regions in Europe and
America north of 30° of latitude to the polar regions contain these
primordial rocks and fossils.
I regard the Menevian of St. David’s as being the most typical,
as regards both physical development and the abundance of organic
remains (individually and specifically). The intricacy of the geo-
logical structure of North Wales renders both the mapping and the
collecting of fossils in the Menevians there far more difficult than
in the St.-Dayid’s promontory, the strike of the beds being more
disturbed in continuity ; but I doubt not that an extensive fauna
is yet to be obtained from the Menevian of North Wales, where the
typical Lower Lingula-flags mantle round the still older Cambrian
masses.
The paleontological value of any group of rocks can only be
arrived at through such analysis as I have here attempted to give ;
it is the census at a given time or age, and from such may be cast or
determined (approximately) the true and absolute value of the zoolo-
gical groups and their distribution through their respective formations.
PLanta.—No traces whatever of plant-remains have occurred in
the Menevian.
Protozoa.—The St.-David’s beds of this age contain all the known
4 species of Protospongia, viz. P. diffusa, P. fenestrata, P. major,
and P. flabellata, the first three of which, as we have seen, are also
Longmynd and Harlech forms. At St. David’s P. fenestrata passes
to the Lower Lingula-flags proper. None have occurred either in the
Menevian or Lingula-flags of North Wales.
Hyprozoa.—No traces. :
Actrnozoa.—Totally unrepresented.
EcurnopERMATA.—Cystidean remains were detected by Mr. Salter
in 1866 at St. David’s; to these he gave the generic name Proto-
cystites. Dr. Hicks subsequently named these fragments P. mene-
vensis, after the horizon in which they occur. These obscure fossils
consist of arm-ossicles and body-plates ; it is the first Cystidean re-
corded. Dr. Hicks has also determined the presence of Dendro-
crinus cambrensis in the Tremadoe rocks of St. David’s, the oldest
Crinoid known in the British rocks.
Aynetipa.—Arenicolites didymus, Salt., A. sparsus, Salt., and Ser-
pulites fistula, Hall, appear to be all that are known of the Anarthro-
ANNIVERSARY ADDRESS OF THE PRESIDENT. ks
poda in the Meneyian beds. ‘The first two are confined ue this
horizon ; S. fistula passes to the Upper Lingula-flags.
Orusracra. —The largest crustacean fauna of the s1x ieaeear of
the lowest Cambrian “dee occurs here. 12 genera and 32 species
characterize the Menevian beds both of North and South Wales.
Agnostus is represented by 7 species, Anopolenus by 3, Conocoryphe
by 7, Paradowides by 3, Holocephalina by 2, and Leperditia by 4
species. ‘These 6 genera are the chief and most largely represented. ,
Arionelius, Erinnys, Microdiscus, and Carausia, each with one species,
are confined to the Menevian beds, and generically characterize them.
The black slaty flags of St. David’s yield the gigantic Paradoaides P.
aurora, Salt., P. Davidis, Salt., and P. Hicksi, Salt.; this last-named
species has been recorded from the Lingula-flags of North Wales under
the name P. Horchhammert. 14 of the 32 species pass to the Lower
Lingula-flags, but none higher; and the Menevian beds are con-
nected below with the Harlech beds and the Longmynd group
through 4 species only, viz. Agnostus cambrensis, Hicks, Conoco-
ryphe bufo, Hicks, Paradoaxides aurora, Salt., and P. Hicksi, Salt.
No Olent occur in the Menevian rocks, although 13 species belong
to the Lingula-flags proper. Olenusis essentially an Upper Lingula-
flag genus, 9 species occurring in that series; and none pass out of
the Lower Cambrian rocks or above the Tremadoc group, where
4 species occur (O. alatus, O. umpar, O. triarthrus, and O. Saltert).
Bryozoa.—No remains of this class occur in the Menevian ; they
first appear in the Upper Lingula-flags under the form of Dictyonema?
Bracuiopopa.—Only 4 genera and 6 species range through the ©
Meneyvian beds, Orthis Hicksvi, Salt., being the only peculiar form.
Lingula ferruginea, Salt., and var. ovalis, Hicks, Obolella maculata,
Hicks, Discina pileolus, Hicks, and Orthis sagitialis, M‘Coy, are asso-
ciated either with the Harlech beds below or the Lower Lingula beds
above. very species occurs in the St.-David’s Menevian beds. It
is not until we rise into the Llandeilo and Caradoc rocks that the
class becomes numerically so distinguished and important a factor
in the Cambrian or Silurian rocks.
LAMELLIBRANCHIATA.—No form known in the Menevian beds.
GastEropopa.—No vestige known in the British rocks of this age.
Preropopa.—Cyrtotheca hamula, Hicks, Stenotheca cornucopia,
Salt., Theca corrugata, Salt., T. penultima, Salt., 7’. menevensis, Salt.,
and J’. stiletto, Salt., or 3 genera and 6 species, are known. 4 of
the 6 species are Menevian only, viz. C. hamula, S. cornucopia,
7’. menevensis, and T’. stiletto. T. corrugata is the only form that
passes to the Lower Lingula-flags above.
Herrropopa.— None known in the Menevian of either South or
North Wales.
CrpHaLopopa.—No species has yet occurred in the British rocks
of this horizon, the only two species in the Lower Cambrian being
those before mentioned, Oyrtoceras precox and Orthoceras sericeum,
both of which are Tremadoc.
Thus we see that, out of the 52 species that constitute the fauna
74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
of the Menevian rocks, 32 are Crustacea—the only other classes
fairly represented being the Brachiopoda, 6 species, and the Ptero-
poda, 6 species. A marked feature is the appearance of Cystidea
(Protocystites) and Crinoidea (Dendrocrinus). Hight whole classes are
entirely unrepresented : the Plante, Hydrozoa, Actinozoa, Bryozoa,
Lamellibranchiata, Gasteropoda, Heteropoda, and Cephalopoda are all
absent. The genera that first made their appearance in the British
Menevian sea were Protocystites, Dendrocrmus, Serpulites, 7 Crus-
tacea (Holocephalina, Entonus, Anopolenus, Arionellus, Leperditia,
Erynnis, and Carausia), Orthis among the Brachiopoda, and 2 Pte-
ropoda (Cyrtotheca and Stenotheca). The other genera appeared for
the first time in the lowest Cambrian of the St.-David’s promontory.
Taste 11.—Menevian.
Oe
4 me Pass to
6 WS Classes. Genera. | Species. | Lower
a & a Lingula.
Plante.
a Br ObOZOa encase ant 1 4 1
Hydrozoa.
Actinozoa.
Echinodermata...... I 1
Nina Shi Ee okbeebodnas 3 3
4 Crustacea Wy... ee 12 32 Vy
Bryozoa.
3 Brachiopoda......... 4 6 3
Lamellibranchiata.
Gasteropoda.
‘ Pteropodarss...-4-c 3 6 4
Heteropoda.
Cephalopoda.
eR iiaileey PRE esto ecoesae 24. 52 a
LINGULA-FLAGS.
The fossiliferous strata lying both above and below the Lingula-
group have of late years been well described and their fossil contents
marked out, the fauna of each group carefully investigated, com-
pared, and catalogued. The Harlech and Llanberris and also the
Menevian beds of South Wales have been exhaustively illustrated
by Hicks and Salter. Upon the Tremadoc group, in North Wales,
the labours of Mr. Homfray, Mr. Ash, and the late Mr. Salter leave
little to be done; subsequently Dr. Hicks investigated the Tre-
madoc and Arenig groups in the St.-David’s promontory, with what
success I hope to show. It must not be forgotten that since the
Geological Survey (thirty years ago) mapped much of North and
ANNIVERSARY ADDRESS OF THE PRESIDENT. 75
South Wales, a great amount of new work has been done by eminent
geologists and paleontologists. Much of the work done by the
Survey has had to be readjusted and reconstructed ; the maps then
prepared with so much skill by Ramsay, Selwyn, Jukes, Aveline,
and others, and which contributed so much to our knowledge, and to
the elucidation of the structure of these intricate regions, are now
in some areas behind the requirements of the age, through the pro-
gress of modern research and nomenclature. The horizons of many
of the lowest fossiliferous groups of rocks as now recognized are
not expressed or delineated on the Survey maps; the now well-
determined Menevian, Tremadoc, and Arenig rocks of North and
South Wales—in other words, all the fossiliferous deposits below
the Llandeilo flags, or between that formation and the base of the
Tremadoc, are not yet delineated on the maps of the Survey. It
may be said by some that the groups of the Harlech, Menevian, and
Lingula-flags may be subdivided and placed upon the Survey maps ;
but the aspect of these beds and the way they occur in the field will
ever prevent this on al-inch scale. ‘Transcendentalism in mapping
has been, and still is, carried to a greater extent and perfection by
the officers of the British Survey than by any other government survey
in the world; and although neither the Tremadoc nor Arenig rocks
are recognized on the maps of the Survey, I believe it will be found
that these formations have received the fullest recognition and atten-
tion in the forthcoming new edition of Prof. Ramsay’s ‘ Geology of
North Wales.’
The Lingula-flags of the Survey and authors generally are equiva-
lent to the Middle Cambrian of Sedgwick, and the Upper Cambrian
of Lyell and Salter; the divisions into Lower, Middle, and Upper
have long troubled systematists in Britain; and the extensive
and almost hypercritical subdivisions adopted have led to much
misunderstanding. ‘The obscurity of these beds in the field, the
smallness of the fauna, and the difference in physical condition in
areas widely separated often render it a matter of opinion where the
lines of demarcation should be drawn, or what should be embraced
by the terms Lower, Middle, and Upper Lingula-flags. The so-called
Middle group has no value whatever, its fauna consisting of five
species only. Three of these are Brachiopoda—Kutorgina cingulata,
Lingulella Davisii, and Lingula squamosa. There is one Trilobite
(Conocoryphe? bucephala, Belt), and also Bellerophon cambrensis, Belt.
These last two forms occur in the upper part of the Dolgelly beds
of that area, and are said to have been associated with Hymenocarts
vermicauda, elsewhere known only in the Lower Lingula-flags.
We must also remember that the ‘‘ Lower Lingula-flags” of Sedg-
wick are the ‘‘ Menevian group” of Salter and Hicks, and that the
“« Wfestiniog group” of Sedgwick constitutes the Middle and Upper
Lingula-flags of Salter. Thus the greatest care is required when
analyzing or correlating these groups, either through their literature
or by research in the field. In the year 1867 the Jate Mr. Belt* con-
* Geol. Mag. vol. iv.
76 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
tributed much to our knowledge of the fauna and geology of the
Lingula-flag series. He was then engaged in investigating the
Dolgelly and other districts, especially with reference to the divi-
sions of the Lingula-flags called the Maentwrog, Ffestiniog, Dolgelly,
and Tremadoc groups, lying between the Menevian and Tremadoc
beds, and occupying extensive areas near Dolgelly and in the
Mawddach valley, also at Maentwrog near Ffestiniog &c.
In 1847 Prof. Sedgwick, on paleontological evidence, removed
the previously named Tremadoe series from the “ Lingula-flags,”
and designated the latter the Ffestmiog group. Salter divided the
Lingula-flags, in 1866, into Lower, Middle, and Upper. Again,
Salter and Hicks, in the same year*, included the Lingula-fiags of
South Wales only in the Ffestiniog group, describing them as being
characterized by “‘ hard siliceous sandstone with grey flaky slate”’ con-
taining “‘Lingulella Davisi.” In character the North-Wales group
of rocks differs altogether from those of South Wales, the arenaceous
flags and shales with Z. Davisi forming only a subordinate part of
a series of fine-grained dark blue and black slates containing many
genera of Trilobites. Mr. Belt restricted the Ffestiniog beds to the
flags containing Lingulella Davisii and the Phyllopod Crustacean
Hymenocaris vermicauda, as originally applied by Sedgwick, and
proposed to name the slates and flags below them the Maentwrog
group, characterized by peculiar Olent. These Maentwrog beds are
exhibited to great perfection at Maentwrog, 8.W. of Ffestiniog.
The blue and black slates occurring above the Ffestiniog series
Belt named the Dolgelly group, with reference to the circumstance
that it is only in this area that both members have been found.
This upper member of the Lingula-flags is characterized by peculiar
forms of Oleni, comprising the subgenera Spherophihalmus, Para-
bolina, &c. These three groups—the Maentwrog, Ffestiniog, and
Dolgelly—are paleontologically and lithologically distinct ; none of
the Trilobita passes from one group to another, peculiar genera occur-
ring in each. Each group also has well-defined lithological charac-
ters. The Maentwrog is readily distinguished by its dark-blue
jointed ferruginous slates; the Ffestiniog by hard micaceous flags
with abundant Lingulella Davis, Hymenocaris, and Conocoryphe ;
and the uppermost or Dolgelly, by species of Agnostus, Olenus and
its subgenera, which are abundant in the soft black slate, which
shows a black streak when scratened. Mr. Belt divided the Maent-
wrog slates into a lower and upper series: the lower are ripple-
marked, and have many Annelide-tracks. They are conformable to
the blue-black Menevian slates which mantle round the Merioneth-
shire anticlinal. This lower group is about 700 feet thick. Olenus
gibbosus, Wahl., and Agnostus pisiformis, Linn. (A. princeps, Salt.),
var. obesus, Belt, occur in the slates. The range between the Eden
and the Mawddach, and near Dolmelynllyn, in the Mawddach, are
the chief localities for fossils. The upper Maentwrog series is
nearly 2000 feet thick. Agnostus princeps is abundant in the flaky
* Brit. Assoc. Reports, 1866.
ANNIVERSARY ADDRESS OF THE PRESIDENT. Th
beds near the summit above Dolgoed ; in thin slaty shales it occurs
in thousands, associated with Olenus truncatus, Ang.; the higher
beds contain O. cataractes, Salt., which replaces A. princeps. ‘This
eroup is completely developed in the Maentwrog district, fine sec-
tions occurring in the Waterfall valley and in the valley running
from Taffarn-helig to Caen-y-coed. Olenus cataractes abounds here.
Lower Frestrinioe Bens.
Thick micaceous grey flags, 2000 feet thick, conformably overlie
the upper Maentwrog beds; the lowest series are bluish-grey slates,
and contain Lingulella Davisu, M‘Coy, with Annelide-tracks ; and
the highest part of the Lower Ffestiniog slates yields Hymenocaris
vermicauda, only known in this division of the Lingula-flags,
Urrrr Frestrnioe.
This group succeeds the Lower series, and is not more than 50 feet
thick, but distinct in fossil contents. The characteristic forms here
are Olenus micrurus and Bellerophon cambrensis. 'This thinly deve-
loped division occurs at Gwern-y-barend, in the Mawddach near
Craig-y-dinas and on Mynydd-Gader.
The river Mawddach cuts through the whole of these beds
between Rhiufelyn and Hatod-fraith, thence ranging across the east
end of Moel Hafodowen and by Pen-y-bryn.
DoLegELLy GRovp.
This uppermost division of the Lingula-flags is physically divided
into two series, lower and upper, the former composed of hard
blue slates abundantly filled with Olenus (Parabolina) spinulosus.
The thickness of this series is about 300 feet.
The upper division differs essentially from the lower. It consists
of soft black slates, with black streak, intensely cleaved and often
pisolitic (fine grains of pisolitic iron-ore). The constant character
of the black streak distinctively marks this group, and in the most
disturbed areas may be relied on as a never-failing criterion of the
upper series. To Mr. Belt is due the determination of this character
over a large area—a fact of inestimable value in the identification
of strata so disturbed and intricately faulted as those round Dolgelly,
Rhobell-fawr, and on Mynydd-Gader. The black shales of Malvern,
overlying the Hollybush Sandstones, and containing Olenus bisulcatus,
Phill., O. scarabeoides, Wabl., O. pauper, O. humilis, Conocoryphe
malvernensis, Agnostus princeps, A. M‘Coyr, &c., belong here; they
underhe the Dictyonema-shales, and are exposed in the valley of the
White-leaved Oak. The upper Dolgelly beds are by far the most
fossiliferous ; and nearly every species in any of the areas is confined
78 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
to this division. The Trilobites in the Dolgelly area are Conocoryphe
abdita, Salt., C. Williamson, Belt, C. longispina, Belt, Olenus
scarabeordes, Sphcerophthalmus (Olenus) alatus, S. (Olenus) humalis,
Phill., Agnostus princeps, Salt., A. trisectus, Salt., and <A. obtusus,
Belt; and, as before stated, the Malvern species are equally restricted.
No one of these occurs below in the Middle and Lower Lingula-flags.
Orthis lenticularis, Dalm., and Obolella follow the same rule all
through the Maentwrog, Ffestiniog, and Dolgelly deposits; the Tri-
lobita that successively appear are closely allied, or belong to the
Agnostide and Olenide; no new types of structure come in, the
fauna being distinctive and similar and homogeneous as a whole.
Dikelocephalus, Conocoryphe, Olenus, and Paradoaides constitute the
natural group or family Olenide ; and the single genus Agnostus is
rich in species. The succeeding Tremadoc and Arenig rocks evidence
great and sudden change, faunal and otherwise, the large Asaphide,
Cheiruride, Trinucleide, and Calymenide then first appearing ;
sixteen genera at once occur in the Arenig, and two in the Tremadoe
(Niobe and Psilocephalus); and we have no proof of any unconformity
in either the North or the South Wales areas: these large forms
come in at once and in vast numbers; and the old forms die out.
Nor have we as yet any evidence of these new and distinct types
having had prior existence in some other area, and migrated into
the Tremadoc or Arenig seas; we know not at present where to look
for evidence of this. Ireland possesses no rocks or fossils of this age
or earlier, Scandinavia none, Western Europe none. America then
possessed gigantic Asaphi ; but in which direction dispersion or dis-
tribution may have taken place we have no trace; although the
evidence tends to show that it must have been towards the east,
or Europe, the main strike of the oldest American rocks being N.H.
and §.W.; while the older groups are greatly developed on the
eastern side of the North-American continent, and there is con-
siderable affinity between the faunas of the two areas, the facies
strongly resembling each other. No migration of an earlier fauna
from one area would fully account for the disappearance of the
earlier gigantic Trilobites (such as Paradoaides, Plutonia) and other
equally characteristic genera (such as Hrinnys, Holocephalina, &c.),
all of which characterize the lowest rocks of Britain, ranging
from the Harlech to the top of the Lingula-flags, call them what
we will.
Salter, as far back as 1853, most carefully described the two groups
(Lower and Upper) of the Lingula-flags in North Wales; he ex-
amined them in their most typical localities, selecting Maentwrog,
Tremadoc, Ffestiniog, Dolgelly, Carnedd Ffiliast, Bangor, &c.
as those places where the Lower division could be best studied.
This he divided into two sections, the lowest consisting of black
pyritous slates, with numerous beds of intercalated sandstones near
the base. These probably in part were Menevian; but the prevail-
ing fossils are Agnostus princeps, Olenus cataractes, and Lingulella
Davisii. (Salter’s species A. princeps is the A. pisiformes, Linn.,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 79
of the Alum slates of Sweden and Norway, which holds the same
position there as in our own area.)
The second division or upper part of the Lower Lingula-flags of
Salter (the typical Lingula-flags) are finely developed in North Wales,
near Tremadoc and Ffestiniog, at Maentwrog, Borth, Marchllyn-Mawr,
Llanberris, Carnedd Ffiliast, Dolgelly, and Trawsfynydd. Cruziana
semiplicata, Hymenocaris vermicauda, Olenus nucrurus, Lingulella
Davisii, and Microdiscus are the leading types of this upper part of
the lower series. Physically these are hard, grey, thick, sandy
beds and flags.
The Upper Lingula-flags of Salter differ essentially from the Lower
Division, consisting of dense black pyritous slates, or black slates with
pyritous bands near the base, with a large fauna differing almost en-
tirely from that of the Lower Lingula-flags; for out of 35 species oc-
curring in the lower group, only 5 pass from the lower to the upper—
namely Agnostus princeps, Microdiscus punctatus, Lingulella Davisir,
L. lepis, and Obolella sagittalis, and this in the same district. At
Tremadoc, Maentwrog, and west of Ffestiniog the beds are rich in
fossils—Olenus alatus, O. scarabeoides, Agnostus primceps, Conoco-
ryphe depressa, C. invita, Orthis lenticularis, and Dictyonema thickly
crowding the beds.
Tt is well known that in 1851 Barrande visited England pur-
posely to compare his fine series of fossils with our types, when he
at once recognized the “ Lingula-flags ” of Sedgwick as the precise
equivalent of his primordial stratum (Etage C). lBarrande also
carried out his comparison and correlation not only with the fauna
of our country, but also between those of the Kuropean and American
continents, with what success the literature and progress of geological
science has shown.
The comparison of the Arenigs of Shropshire (Stiper stones) and
Westmoreland (Skiddaw) will form an important feature for our
consideration.
The close analyses of the Lower and Upper Lingula-flags must be
taken separately. The faunas of the two differ remarkably ; and only
8 species connect them—namely 5 species of Trilobita (Asaphus
princeps, A. trisectus, A. Salter, Microdiscus punctatus, and Para-
doxides Hicksii) and 3 of Brachiopoda (Lingulella Davisu, L. lepis ;
and Orthis sagittalis). The Middle Lingula-flags of some authors con-
tain also only 5 species :—1 Trilobite, Conocoryphe bucephala, Belt ;
3 Brachiopoda, Kutorgina cingulata, Belt, Lingula squamosa, Holl,
and Langulella Davisii; with Bellerophon cambrensis, Belt. Two
of the five species appear to be confined to this horizon, viz. Lingula
squamosa and Bellerophon cambrensis. This fauna is too small to
be of any value for our present purpose.
Pranta.—No trace of any kind.
Prorozoa.—Thesponge Protospongia fenestrata, Salt., passes up from
the Menevian and Harlech beds at St. David’s to the Lower Lingula-
flags. ‘This species has the longest range of the four known forms ;
but none of the four ranges higher.
80 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
Hyprozoa.—No appearance; none occur before the Arenig rocks
were deposited.
Actinozoa.—No traces of Coelenterata in any form.
KcuinopERMATA.—N one occur in the Lingula-flags. The cystidean
Protocystites menevensis is Menevian only; and the first Crinoid
appears in the Lower Tremadoc of Ramsey Island.
ANNELIDA.—Three genera and three species. The characteristic
Cruziana semiplicata, Salt., hitherto has only been found in the Cam-
brian grits of the Bangor area, near Cwm Grainog and Carnedd-
ffiliast, in North Wales (Lower Lingula-flags of the Survey).
Specimens of this Cruziana or an allied species have occurred
below the Stiper stones in the Shelve country, W. of the Longmynds.
Scolicoderma tuberculata, from Pentre-felen quarry, near Wem
Gate, Caernarvonshire, and Helminthites from the Maentwrog sand-
stones. None of these forms occurs out of the Lower Lingula-flags.
CrustacEa.—This class is nearly equal in zoological value to what
it is in the Menevian. 9 genera and 25 species have been described :
14 of the same species appeared before in the Menevian, and therefore
occur in both formations ; 6 species (Agnostus princeps, A. trisectus,
Anopolenus Salterr, Microdiscus punctatus, Paradoaides aurora, and
P. Hicksw) pass to the Upper Lingula-flags. Like the Menevian
beds it is the home of Agnostus, 6 species of that genus occurring ;
but only 2 are peculiar or confined to the Lower Lingula-flags,
viz. Agnostus limbatus and A. nodosus; besides these Olenus cata-
ractes, Salt., O. micrurus, O. gibbosus, and O. truncatus? are also
Trilobites confined to this horizon; the Phyllopod Hymenocaris
vermicauda essentially characterizes the Lower Lingula-flags; so
that, large as the Crustacean fauna appears (25 species), there are
only 8 that are really Lower-Lingula species; the remaining 17
ally the Lower Lingula either with the two formations below or
with the Upper Lingula and Tremadoc above. The 7 typical spe-
cles are given above. The genus Conocoryphe, which is very largely
represented in the Lower Cambrian rocks (by no less than 21 spe-
cies), has no distinctive or peculiar form in the Lower Lingula-fiags ;
4 occur, but none are restricted. They are Conocoryphe applanata,
C. bucephala, C. humerosa, and C. variolaris. 9 species of the
genus Conocoryphe occur in the Upper Lingula-flags; and, as we
shall see, this division possesses also more peculiar forms and a
larger specific Crustacean fauna than the Lower Lingula-flags, but
fewer genera. ‘The species of Conocoryphe and other genera are as
follows—Agnostus obtusus, A. princeps, A. trisectus, A. Turneri,
A. venulosus, Ampyx prenuntius, Anopolenus Salteri, Conocoryphe
abdita, C. bufo, C. depressa, C. invita, C. malvernensis, C. longispina,
CO. Plantii, C. simplex, C. Williamsoni, Microdiscus punctatus, Olenus
bisulcatus, O. flagellifer, O. (Sphceerophthalmus) humilis, O. obesus,
O. pauper, O. pecten, O. (Peltura) scarabeoides, O. serratus, O. spi-
nulosus, Paradoxides aurora, and P. Hicksiit, also Primitia sol-
vensis,
Bryozoa.—None have yet appeared.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 8I
Bracutopopa.—Lingulella, Obolella, and Orthis are the only 3
genera in the Lower Lingula-flags. The 5 species are Lingulella
Davisu and L. lepis (both ranging to the Arenig), L. ferruginea,
Obolella maculata, and Orthis sagittalis. The last named is also
Tremadoc.
LAMELLIBRANCHIATA.—None known below the Lower Tremadoc,
where 3 new genera and 12 species suddenly appear; they will be
noticed under the Lower Tremadoc beds.
GasrERopopa.—None occur beneath the Arenig rocks.
Preropopsa.—Theea corrugata, Salt.,and 7’. obtusa, Salt., are the
only 2 species that occur. The last named is confined to the Lower
Lingula-flags.
Hereropopsa.—None below the Middle Lingula-flags ; and the only
species occurring therein is Bellerophon cambrensis, Belt.
CrpHatopopa.—None have yet appeared below the Upper Tremadoc,
where the oldest forms known occur.
The fauna of the Lower Lingula-flags is expressed in the follow-
ing Table; and it will be seen in the passage column that only 8
species pass to the Upper Lingula-flags. They are Agnostus prin-
ceps, A. trisectus, Anopolenus Salieri, Microdiseus punctatus, and
Paradoxides Hicks, Lingullela Davis, L. lepis, and Orthis sagittalis.
Only 2 species are believed to connect the Middle and Lower Lin-
gula-flags—Oonocoryphe bucephala, Belt, and Lingulella Davisn,
M‘Coy. Indeed the whole fauna of the middle division only amounts
to 5 species—the two just named, and Kutorgina cingulata, Bil.,
Lingula squamosa, Holl, and Bellerophon cambrensis, Belt.
Nine entire classes are unrepresented in the Lower Lingula-flags,
as shown in the Table.
Taare IT1.—Lower Lingula-flags.
Pass up Pass to | Pass to
from Classes. Genera. | Species. | Middle | Upper
Menevian. Lingula-| Lingula-
flags. flags.
Plante.
7 IPROUOZOR) Suresh sca ceewe nes if 1
Hydrozoa.
Actinozoa.
Echinodermata.
Annelida ....... Rag Wane 3 3
rie (AAU TUSUACEA cose ceo hesasse cess 9 25 s a
Bryozoa.
: iBrachiopodace: 8. o.<..5- 3 5 a :
Lamellibranchiata.
Gasteropoda.
Pteropodarss se.) 0see=- 1 2
Heteropoda.
Cephalopoda.
1 nase gh aM Cee ee ta 17 36 z z
82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Upper LINGULA-FLAGS.
Prantz.—None known.
Prorozoa.—None occur.
Hyproz0a.—Dretyonema sociale occurs abundantly in the grey and
dark shales of Keys End Hill, Malvern, andin North Wales. Whether
Dutyonema should be placed with the Hydrozoa or Bryozoa is still
a doubtful question. Salter in 1857 separated this genus from
Kjerulf’s genus Fenestella and also from Hall’s genus Graptopora.
Actiyozoa.—None.
Koutyopermata.—None.
ANNELIDA.—2 genera, Scolicoderma antiquissimum, Salt., and Ser-
pulites fistula, Holl. The Hollybush sandstone of the Malverns is
characterized by the two Annelides above named; the Hollybush
beds of the Wrekin also contain Annelide remains. S. fistula first
appears in the Menevian beds. Whatever may be the age of the
Hollybush sandstones, these two species occur in the Malvern area,
at the base of the Upper Lingula-flags.
Crustacea.—No less than 30 species represent the following eight
genera—Agnostus 5 species, Ampyw 1, Anopolenus 1, Conocoryphe 9,
Dikelocephalus 2, Microdiscus 1, Olenus 9, Paradowides 2*. 4 species,
viz. Agnostus princeps, Ampyx prenuntius, Conocoryphe depressa, and
Olenus alatus, pass from the Upper Lingula-flags to the Lower Tre-
madoc’; and 20 species are confined to this horizon. Thus the Upper
Lingula-flags through their Crustacea become of much importance,
and the few (4) that pass to the Tremadoe clearly show the strati-
graphical value of the Lingula group and its distinctness. It may be
worth stating that 4 species in the Upper Lingula-flags also occur
in the Menevian; they are Anopolenus Salteri, Microdiscus punctatus,
Paradoxides aurora, and P. Hicksiv; only 2 species of the 4 that
pass from the Upper Lingula-flags to the Tremadoc extend up into
the Upper Tremadoc, namely Agnostus princeps and Ampyx pre-
nuntius.
Bryozoa.—Dictyonema sociale, Salt., is the only Bryozoon known
in the Upper Lingula-flags ; it passes to the Lower Tremadoce, both in
the North and South Welsh areas, at Tremadoc and St. Dayid’s; it is
highly characteristic of the pale Dictyonema-shales that overlie the
black shales in the valley of the White-leaved Oak at the southern end
of the Malvern ranget. These black and pale greenish Upper Lin-
gula shales are about 500 feet thick, and contain a singular fauna
of Crustacea and Brachiopoda. Prof. Phillips first noticed these
shales and their fossil contents. The Crustacea are Conocoryphe
malvernensis, Phill., Olenus bisulcatus, Phill., O. humilis, Phill., O.
spinulosus, Phill., and O. pauper, Phill., Spherophthalmus pecten,
Salt., Agnostus M‘Coyr?, Salt., and A. princeps ; the Brachiopoda are
* For list of the species see p. 80, last paragraph in the Lower Lingula-flag
division.
+ It is possible that Kjerulf’s Fenestella socialis from Scandinavia may be our
Dictyonema; Eichwald’s Gorgonia flabelliformis, although much larger, is almost
identical; Mr. Salter, however, established its generic distinctness.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 83
Langula pygmeea, Salt., Obolella Salteri, Holl, and Spondylobolus, sp. ;
many of these are peculiar to the Malvern area. Dr. Holl* in 1865
described the geological structure of the Malvern Hills and adjacent
districts, placing these shales in the Upper Cambrian, the Hollybush
sandstone being the base or lowest known sedimentary rock in the
Malvern area. Whether Dictyonema should be classed with the
Bryozoa or Hydrozoa is still a doubtful question.
Bracurorpops.—Only 5 genera and 8 species occur in the Upper
Lingula beds—-Kutorgina cingulata, Lingulella Davisii, L. lepis,
Langula pygmea, Obolella plicata, O. Saltert, O. sagittalis, and Orthis
lenticularis. 6 pass tothe Tremadoe rocks—Kutorgina cingulata,
LInngulella Davisti, L. lepis, Obolella plicata, O. sagittalis, Orthis
lenticularis ; only 2 species are really restricted to the Upper Lin-
gula-flags, Lingula pygmea and Obolella Saltert. No zoological
value can therefore be attached to the Brachiopoda, as all the species
but 2 occur both below and above the Upper Lingula-fiags.
LAMELLIBRANCHTATA.—None have as yet been detected.
Gastrropopa.—None known below the Arenig.
Prrropopa.—Of the 4 genera and 17 species that range from the
Longmynd group of St. David’s to the Upper Tremadoc no form has
yet been discovered in the Upper Lingula-flags.
Hzreropopa.—None have occurred, although 5 species range
through the Lower Cambrian rocks. Theso-called Middle Lingula-
flags have yielded one species, Bellerophon cambrensis, Belt, which is
the first known species on record.
CrpHatopopa.—None of any type. No species occur below the
Lower Tremadoc. The entire Cephalopod fauna of the Lower Cam-
brian rocks consists only of 1 genus and 2 species below the Arenig
rocks, Orthoceras precow, Salt., and O. sericeum, Salt.; in the Upper
Tremadoc these increase to 5 species.
Between the close of the deposition of the Menevian rocks and the
close of the Upper Lingula-flags, 10 new genera appeared, viz. 3 An-
nelida, 1 Bryozoon, 4 Crustacea, and 2 Brachiopoda+, succeeded by
13 new species in the Tremadoc(Hchinodermata 2 species, Crustacea 4,
Lamellibranchiata 5, Cephalopoda 2 species). The known newly intro-
duced genera in the Lingula-flags were, Oruziana, Scolicoderma, Hel-
minthites, Dictyonema, Parabolina, Dikelocephalus, Peltwra, Hymeno-
caris, Lingula and Kutorgina. Only 1 of these (Lingula) lived on
after the deposition of those sediments we term Lingula-flags ; this
genus has appeared in almost every successive marine formation.
The Lower Lingula beds have yielded 17 genera and 36 species, and
the Upper Lingula-flags 16 genera and 41 species, showing a generic
loss or dying out of 7 genera in their upward succession; they ap-
pear to be Protospongia, Cruziana, Helminthites, Anopolenus, Holo-
cephalina, Hymenocaris, and Leperditia.
* Quart. Journ. Geol. Soc. vol. xxi. 1865, pp. 72-102.
t Cruziana (semiplicata), Scolicoderma (tuberculatum and antiquissimum),
Helminthites (sp.), Dictyonema (sociale), Hymenocaris (vermicauda), Olenus (cata-
ractes), Dikelocephalus (celticus and discoidalis), also Carausia (menevensis), with
Lingula and Linguletla.
84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
The two accompanying small Tables (III. & IV.) relate to the dis-
tribution of the fauna of the Lower and Upper Lingula-fiags, with the
number of genera and species that pass to the Lower and Upper Tre-
madoc. Nine whole classes are unrepresented in each division ; only
2 classes, indeed, in either have real value, the Crustacea and Brachio-
poda. I regard the Annelida as being wholly doubtful, so far as
regards species: their presence and influence is manifest every where
through the slates and flags of the lowest Paleozoic rocks ; but the
fragmentary condition of the remains, as well as the uncertainty
relative to their development and history, almost sets aside their
numerical value as species in evidence.
In the Lower Lingula-flags the 25 species of Crustacea stand alone ;
and, with the exception of Hymenocaris vermicauda, Leperditia
Hicksii, and Primitia solvensis, all are Trilobita. Five species,
all Trilobites, pass to the Upper Lingula-flags. The Upper Lingula-
flag table is even more significant ; for every one of the 30 species of
Crustacea belongs to the group of Trilobita, and only 2 species pass
to the Upper Tremadoc, Agnostus princeps and Ampyx prenuntius,
and not one to the Arenig, from the Lingula-flags.
The left-hand column in all the tables shows the number of genera
and species that pass up from the next underlying or older formation,
the upper figure enumerating or expressing the number of genera,
and the lower denoting the number of species in each class; the
same plan is appled to the genera and species that pass up into the
several formations as the case may be, and as expressed in the head-
ings of the columns. The column headed classes and the two suc-
ceeding, marked genera and species, speak for themselves.
Taste 1V.—Upper Lingula-flags.
cau Pass to | Pass to
Lower Classes. Genera. | Species. pels: a s be
ew madoc. | madoc.
| Plante.
Protozoa.
Hydrozoa.
Actinozoa.
Echinodermata.
Ammelicda; Wa osandermascer eee: a: 2 2
g C@ristacen era.csesecte cect 8 30 4 Z
SEV OZOAR ind oenatissemein ae 1 1 7
3 iBrachiopodda):.n.5-ses-5).26ees 9) 8 i 2
Lamellibranchiata.
Gasteropoda.
Pteropoda.
Heteropoda.
Cephalopoda.
Zech br oh gigi apne tee tar 16 41 nie 7
ANNIVERSARY ADDRESS OF THE PRESIDENT. 8 5
Lower AND Upper TREMADOC.
Prior to the year 1865 little or nothing was known of the Tre-
madoc rocks in the promontory of St. David’s; but in North Wales
they had been well studied by Sedgwick in 1847, and by Salter in
1857; and in 1866 Salter and Hicks catalogued all the species
known up to that time*. Doubtless the Lower Tremadoc series
are a continuation and natural close of the Upper Lingula-flags or
Ffestiniog series (the Middle Cambrian of Sedgwick). ‘The strict
agreement, however, between the North- and South- Wales Tremadoc
faunas was not thoroughly understood until Dr. Hicks in 1873 care-
fully described and correlated the paleontological relations that
exist between the typical North- and South-Welsh areas. The
researches of Dr. Hicks into the Tremadoc fauna of the mainland
of St. David’s and that of Ramsey Island made us then familiar
with the physical relation and paleontological connexion between
the two areasy. The prior and incomplete observations of Hicks
and Salter in 1866 at Ramsey Island relative to the presence
there of the Tremadoc rocks, Dr. Hicks in 1872 fully confirmed,
being able to show their succession to, and conformable position
with, the hard siliceous flaggy Lingula-flags. In this research he
was assisted by three able and competent observers, Messrs. Hom-
fray, Lightbody, and Hopkinson, the last-named naturalist sub-
sequently contributing largely to the Arenig Hydrozoa from the
same area. Dr. Hicks’s labours further resulted in Mr. Davidson’s
learned paper upon the earliest British Brachiopoda, which con-
tains a valuable table showing the distribution of all the known
species of that class in these oldest British rocks (Harlech to Tre-
madoc).
Since the labours of Dr. Hicks in Wales, another important ad-
dition has been made to our knowledge of the distribution and
fauna of the Lower Tremadoc rocks of the Wrekin area, through the
careful research of C. Callaway, Hsq., F.G.S. Mr. Callaway cor-
rected errors made by the Survey, Sir R. Murchison, and Mr. Salter
in the reading of the Harnage and Shineton beds in Shropshire. He
described the Lower Paleozoic rocks that range from Wellington
to Kenley (N.E. to 8.W.). He paid no critical attention to rocks
newer than the Caradoc; but he greatly changed the previous views
as to the reading and structure of the county§. Mr. Callaway
clearly showed that the Shineton Shales are of Lower-Tremadoc
age, and that the “quartzite” rock that les between the Shine-
ton Shale and the Wrekin represents the Hollybush Sandstone of
Malvern, which there underlies the black shales with Olenz, the
equivalents of the Upper Lingula-flags. The determination by
Mr. Callaway of the presence of a Tremadoc fauna in England is of
high importance; and, singularly, most of the Shineton Tremadoc
* British Association Report, 1866.
Tt Quart. Journ. Geol. Soc. vol. xxix. p. 39 (1873).
+ Geol. Mag. vol. v. (1868) pp. 3803-315.
§ Callaway, Quart. Journ. Geol. Soe. vol. xxxiii. pp. 652-672.
MOt, XXX VIT. 4 h
36 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
species are new, and also many of the genera. The species as-
signed by the author as having most zoological value are Conocoryphe
monile, Salter, Olenus Saltert, Call., Olenus triarthrus, Call., Agnostus
dux, Call., Lingulella Nicholsoni, Call., Obolella sabrine, Call.,
Asaphus (Asaphellus) Homfrayi, Salt., Asaphus (Platypeltis) Crofti,
Call.
Mr. Callaway also draws comparisons between the Shineton,
Pedwardine, and Malvern series, showing their relations and affinities.
All the species in the Shineton Shales are new except three, viz.
Conocoryphe monile, Salt., Asaphus (Asaphellus) Homfrayi, and
Dictyonema sociale; the fauna is therefore nearly unique. Mr.
Callaway suggests that the Shineton Shales may be passage-beds
between the Lingula-flags and the Lower Tremadoc: the presence
of Dictyonema sociale strengthens this view; it is an Upper Lin-
gula-flag species at Malvern, Pedwardine, and North Wales in
many places, also a well-known Tremadoc form in the latter
area. Mr. Callaway ably discusses the physical features of the
Shineton area. He describes fourteen new species, and establishes
two subgenera of Trilobites, Asaphellus and Platypeltis, and two
genera, Conophrys and Lichapyge ; he also determines and describes
a remarkable Cystidean, possessing a slender crinoidal-like stem and
simple calicular pinnule, which he names Macrocystella Marie. At
present we know of no true Tremadoc rocks in the Stiperstones area ;
nor, indeed, are we sure of the presence of the true Lingula-flags in
that district west of the Longmynds, unless the Stiperstones them-
selves represent them; but of this we have no organic proof, the
series succeeding being Arenig or Skiddaw, formerly mapped and
named Lower Llandeilo by Sir Roderick Murchison and the Survey.
Mr. Callaway believes from recent research that the quartzites of
the Stiperstones are of Arenig age, and therefore distinct from the
quartzites of the Wrekin, deducing his opinion from the fact that
when they are conglomeratic the pebbles in the Arenig quartzites
are mainly quartz, while the included fragments of the Wrekin
quartz rocks are felsitic. Again, Mr. Callaway believes that he has
detected the Shineton Shales (Lower Tremadoc) at the base of the
escarpment of the Stiperstones dipping under the Arenig series in
the same direction as the rocks of that formation, 2.e. W.N.W.
There is little or no specific paleontological affinity or com-
munity between the Tremadoc and Arenig groups in any known
area in North or South Wales, although they are everywhere con-
formable. No Tremadoc rocks have yet been proved to occur above
the Lingula-flags in the passes of Llanberris and Nant Francon or
the adjoining regions, where the latter rocks are so finely and fully
developed ; neither is it yet quite certain that they occur in An-
glesey. <A few fossils lately found by Professor T. M‘K. Hughes
lead to a strong suspicion that the northern half of the island may
yet yield a Tremadoc fauna. The singular Trilobite, Neseuretus
ramseyensis, Hicks, found by Professor Hughes at Ty-hen near Llan-
erchymaedd, has not hitherto occurred in North Wales, but only on
Ramsey Island and at Tremanhire (St. David’s); and other remains
ANNIVERSARY ADDRESS OF THE PRESIDENT. 87
occur with this form, furnishing strong evidence that the Tremadoc
rocks extend as far N.W. in Wales as Anglesey: the above-men-
tioned species has not occurred in the classical Tremadoc area, either
in the lower or the upper division of the group. The presence of
the Arenig beds in Anglesey favours the belief that the Tremadoc
may also occur in the island.
The Tremadoce slates, now so well known in the two classical
Welsh localities, viz. Tremadoc in North, and St. David’s in
South Wales, are so rich in conspicuous forms and well-determined
species that we readily recognize and place them in two distinct or
separate horizons or zones. ‘heir true position in North Wales,
between the Lingula-flags below and the Arenig group above, was
clearly shown and fixed by the distinguished Cambridge Professor
in 1851. Their base was an easier line to trace than their passage
above into what was then a group of rocks believed to be almost
unfossiliferous. Small indeed was the fauna known to Sedgwick
and Salter in 1843, when, at Tai-hirion, west of Arenig Mountain,
they collected the two characteristic fossils Ogygia Selwyn and
Calymene parvifrons. These two species formed the mental basis
of Sedgwick’s Arenig, and determined the top of his Tremadoc
group till better worked out. Now the Tremadoc fauna of North
Wales consists of 42 species, of South Wales 30, and of Shropshire
(Shineton) 16. The Arenig group numbers 62 genera and 149
species; or 97 species occur at St. David’s, 74 in the Skiddaw beds
of Westmoreland, 36 in the Stiper-stones area, 34 in North Wales.
These have nearly all been described since the far-seeing eye of
Sedgwick determined the stratigraphical place of the groups on
physical grounds. We owe the description of the species to Dr. Hicks,
Mr. Salter, Professor M‘Coy, and Messrs. Hopkinson, Lapworth,
Nicholson, and Davidson. Guided by mineral or physical characters
alone, the line of separation between the Lingula-flags and Lower
Tremadoc would probably be drawn immediately above the hard
grey arenaceous so-called Middle Lingula-flags, in the typical Tre-
madoe area, where Lingulella Davisit ceases to be an abundant and
characteristic fossil ; but zoological conditions forbid this ; the ‘ black
slates’ that succeed the “hard grey series,” possess a recurrent
generic fauna from the lower zones, including Conocoryphe depressa,
Dikelocephalus?, and Agnostus princeps, with Orthis lenticularis,
the two latter in millions. The cliff of Ogof-ddu, near Criccieth,
and the jutting promontory of Craig-ddu exhibit a complete section
from the Lingula-flags to the Upper Tremadoc slates, the character-
istic Orthis lenticularis marking by myriads the junction of the
Middle Lingula-fiags and the Upper Black pyritous slate. No Upper
Lingula-flag section in Wales is more prolific in life: Conocoryphe
abdita, Salt., and two other species, Dikelocephalus celticus, Salt.,
D. discoidalis, Salt., Agnostus princeps, and Orthis lenticularis
dispel all doubts as to age or horizon; but the Tremadoc fossils do
not occur at Ogof-ddu; the fossiliferous zones must be sought for in
the sections at Penmorfa, Borthwood, Moel-y-gest, dc. near Port-
madoc (places rich in characteristic species), and also across the
estuary from Aber-ai, by Dudreath, to Cae-lago, near Maentwrog.
h2
88 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
These are the chief localities whence the history of the Tre-
madoe rocks of North Wales has been drawn and deduced, from
which also their remarkable fauna has been disentombed, and that
mainly through the instrumentality of Mr. David Homfray and Mr.
Ash of Portmadoe, the late Mr. Salter, and the old collector for the
Survey, Mr. Gibbs.
The careful and thorough examination of North and South Wales
that has of late been made by so many able observers, has clearly
shown the perfect sequence and agreement in stratigraphical suc-
cession between the whole of the groups ranging from the Har-
lech and Longmynd strata to the Llandeilo; this is complete for
South Wales in the St.-David’s promontory as one continuous and
ascending section, with no break in continuity. It is not so clear
or complete a sequence in North Wales, where the chief localities
for the Tremadoc and Arenig groups are more widely separated,
both formations being only developed in two counties in North
Wales, viz. Merionethshire and Caernarvonshire—the Lower Tre-
madoce series chiefly at Penmorfa, Borthwood, and Llanerch in
Caernarvonshire, and in Merionethshire at Cae lago near Maentw-
rog and at Tyn-y-llan. The Upper Tremadoc rocks, on the contrary,
are best developed in Merionethshire at Tuhunt-y-bwlch, Penclo-
gwyn, and Garth, whilst Moel-y-gest is the only locality in Caernar-
vonshire where they occur. The Arenigs, which also occur only in
the same counties, I shall have occasion to refer to at considerable
length when speaking of the distribution of the species.
The discovery near St. David’s, by Hicks and Salter, of Tremadoc
slates equivalent to those of North Wales threw new light upon the
history of that remarkable promontory. Not only are these slates
the same as those of Merioneth and Caernarvonshire, but a large
number of additional species of much interest have been added to the
whole fauna. In 1866* Messrs. Hicks and Salter published the results _
of their researches at St. David’s, giving a list of the species dis-
covered by them. Since then Dr. Hicks has reaped a large harvest
of new forms from these rocks, thus adding to the history and
paleontology of that area—no less than thirty species having
occurred to him. These were obtained from three distinct loca-
lities—the first on the north-eastern coast of Ramsey Island ;
the second at the northern extremity of Whitesand Bay, and ex-
tending 4 miles in a north-easterly direction beneath the Arenig
rocks; the third at Tremanhire, an extensive area or tract 5 miles
east of St. David’s, thus showing extensive geographical distri-
bution. The Ramsey-Island section is stratigraphically complete,
having for its conformable base the Lingula-flags full of Linguiella
Davisit ; and upon the intervening Tremadoc rocks, here 1000 feet
thick, succeed the Arenigs, thus here, as at Whitesand Bay, affording
clear proof of the intercalated position of the Tremadoc group. In
North Wales no Arenig rocks are known to rest directly upon the
Tremadoc anywhere. Dr. Hicks obtained in all 29 species from
the Ramsey-Island section, 24 of which were new; and 15 occurred
at Tremanhire, inland, east of St. David’s.
* Brit. Assoc. Report, 1866, p. 182.
ANNIVERSARY ADDRESS OF THE PRESIDENT, 89
The Tremadoc rocks of Whitesand Bay also rest conformably
upon the Lingula-flags, and underlie the Arenigs, as at Ramsey
Island; they strike north-east for 4 miles towards Abereiddy Bay.
The third exposure, at Tremanhire, shows the same stratigraphical
relations and succession, and has yielded fifteen out of the 30
new species described by Hicks as occurring at Ramsey Island.
This patch is now an isolated inlier surrounded by Lingula-flags and
Menevian beds, and with a large area of Longmynd rocks to the west.
The Pre-Cambrian ridge and Longmynd series now divide or sepa-
rate the two Tremadoc areas, which must have been once conti-
nuous. Dr. Hicks believes that the conditions under which these
rocks at St. David’s were deposited were intermediate between those
of the shoal and shallow water in which the Lingula-flags were
deposited, and those of the deeper sea from which the finer muddy
deposits of the Arenig slates were thrown down, and that this was
probably one of the causes of the appearance in them of so varied a
group of organisms.
There is some difficulty in comparing the Tremadoc rocks of
North with those of South Wales. At St. David’s they are so inti-
mately connected with the underlying Lingula-flags and overlying
Arenig series that the boundary-line is almost arbitrary. Palseon-
tologically they appear to be on the same horizon as the Lower
Tremadoc series of North Wales, the chief trilobite Niobe Homfrayt
with Lingulella Davisti and L. lepis connecting them. Yet the
mass of the faunas are entirely distinct, for out of the 42 North-
Wales and 30 South-Wales forms only the 3 above named are com-
mon to both.
Thus out of the 4 North-Wales and 7 South-Wales Trilobita
only 1, Mobe Homfrayi, connects the two areas. Of the 4
genera and 9 species of Brachiopoda occurring in both areas only
2 species connect them, viz. Lingulella Davisii and L. lepis; and
more remarkable still is the occurrence in Ramsey Island of the
earliest known Lamellibranchs in Britain, if not in Hurope. The
Lower Tremadoc beds in that island have yielded 5 genera and
12 species, the first representatives known of that order; 6 of
the same species occur inland at Tremanhire. ‘Three of these genera
belong to the Arcide, and one probably to the Anatinide ; prior to
this discovery Jtedonia, Ribieria, and a species of Palearca were the
oldest forms known, and were obtained from the Arenig beds at Lord’s
Hill, Shelve. The last-named genus has been extracted from Lower
Silurian rocks in Spain, Bohemia, France, and Devonshire. These
bivalves are also associated with the earliest known Crinoid and
Starfish, Dendrocrinus cambrensis and Paleasterina ramseyensis. Still
more significant zoologically is the presence of a new genus with
four species of Trilobita, which Dr. Hicks has named Neseuretus.
This large and singular genus seems to have affinity with Drke-
locephalus through its pygidium, with Calymene and Homalonotus
through the thoracic segments, and with the Conocephalide
through the glabella. The four species and one variety are all
confined to the Lower Tremadoc rocks of Ramsey Island and
Tremanhire on the St.-David’s promontory. None had occurred in
go PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
North Wales until Prof. Hughes discovered portions of one in Angle-
sey. If any other Trilobite were required to establish paleontological
relationship between the Tremadoc rocks of North and South Wales
it would be Angelin’s genus WMiobe ; and Dr. Hicks has obtained, both
from Ramsey Island and Tremanhire, a new and splendid species
(Niobe menaprensis), greatly exceeding in size the characteristic
Niobe Homfrayt from Penmorfa and Tremadoc. Niobe is not
known out of the Tremadoc group. The South-Wales beds do not
possess so numerous an assemblage of pelagic Mollusca as those of
North Wales: 9 species of Pteropoda (Theca Davisii, T.
opercula, Lower Tremadoc only, 7. arata, T. bijugosa, T. cuspi-
data, Lower and Upper, and 7’. alata, T. simplex, and T’ tri-
lineata, with Conularia Homfrayr) are Upper Tremadoc; and 5
Heteropoda (Bellerophon arfonensis, B multistriatus, B. ramsey-
ensis, B. solvensis, and B. shinetonensis) range through the Trema-
docs; but Theca Davisii, Bellerophon ramseyensis, Hicks, and B.
solvensis, Hicks, are South-Wales species, the mass occurring in the
typical Tremadoc area in North Wales. Associated with Vzobe
menaprensis and the Nesewretr no less than 19 species occur,
including the 12 Lamellibranchs and 5 Brachiopoda, viz. Lin-
gulella Davisu, Lingula petalon, Obolella pheata, Orthis Carausit,
and O. menapiw, 29 of the 31 being described by Hicks.
Dr. Hicks believes that the lower portion of the St.-David’s
Tremadoc rocks and the upper black slates of the Lingula-flags of
North Wales were deposited contemporaneously. This may well be,
looking at the remarkable difference existing in the faunas of the
two areas, so few species being common to or uniting the two groups,
and difference of depth at the time of deposition. Again, the
absence of the fine black slates in the Upper Lingula-flags of St. °
David’s, so characteristic of the North-Wales and the Malvern beds,
may be due to depth, shallow in one region and deep in the other.
The Tremadoc series is divided into three groups by Dr. Hicks,
the lowest at St. David’s consisting of grey, fissile, or flaggy sand-
stones. Exposed at Ramsey Island, Tremanhire, and Llanveran, a
peculiar assemblage of fossils occurs in this area, new and different
from that of North Wales:—Davidia, Glyptarca, and Palcearca,
being the earliest bivalves known; the earliest Crinoid, Dendrocrinus
(unless Mr. Callaway’s genus Macrostella from the Shineton area
should be earlier in time); and the first known Asteroid, Paleasterina
ramseyensis, Hicks. The Middle Tremadoc of Hicks is equivalent to
the passage-beds between the Lower and Upper series of Salter, con-
taining Cheirurus Frederici, Conocoryphe verisimilis, C. vewata, and
Asaphus Homfrayi,—the upper member, consisting of iron-stained
slates and flags at Penclogwyn, Garth, Dudreath Tuhwnt-yr-
bwlch, &c., in the Portmadoc area being characterized by Angelina
Sedgwickit, Lingulocaris lingulecomes, and Conularia Homfrayt.
The distinctness of the Tremadoc from the Lingula-flags below is in
all areas the same; only 8 species out of 65 known forms in the
former pass up to the Tremadoc, which possesses a fauna of 34
species; these are Agnostus princeps, Ampyw prenuntius, Conocoryphe
depressa, Lingulella Davisit, L. lepis, Orthis lenticularis, Obolella
ANNIVERSARY ADDRESS OF THE PRESIDENT. gt
sagittalis, and Diciyonema sociale. 42 species are known in North
Wales, and 30 in South Wales; yet, as before stated, only 3 species
are common to both districts—Mobe Homfrayi, Lingulella Davisi,
and ZL, lepis.
It must be observed that no species of true Graptolite is known
in the Tremadoc rocks, none being really known below the Arenig
in Britain, Europe, or America. Doubtless the whole Arenig series
is more closely allied to the succeeding and overlying Llandeilo than
to the underiying Tremadoc; it is certainly so as exhibited in the
South-Wales promontory, where both groups are typically developed
and succeed each other in one continuous and conformable section ;
yet there is perhaps no greater change or paleontological break be-
tween any two conformable British groups than between the
Tremadoc and Arenig, the rich Hydrozoal fauna coming in at the
close of the former and commencement of the latter. The change
in the physical conditions of the sea and sea-bed at the close of the
Tremadoc period was favourable to the development of this division
of the Coelenterata.
The most characteristic of all the fossils of the Lower Tremadoc
are Miobe Homfrayi, N. menapiensis, Psilocephalus wnnotatus, with
Angelina Sedgwicku and <Asaphus affinis in the Upper Tremadoc;
these five species are met with wherever the Tremadoc rocks are
well seen. <Agnostus princeps, so abundant in the Upper Lingula-
flags of North Wales, is not known in the St.-David’s Tremadoc
sections, and is of the rarest occurrence in the North-Welsh classical
localities ; with Agnostus the characteristic Lingulella (L. Davisir)
dwindles away, and seems to be replaced by the small but equally
gregarious L. lepis.
The true Upper Tremadoc series is characterized by many new
species. Niobe Homfrayt, Psilocephalus innotatus, and P. inflatus
no longer exist as species, but are replaced by Asaphus Homfrayt
and Angelina Sedgwicki; Cherurus Predericc at Garth, Llanerch,
Penclogwyn, Portmadoc, &c., ranges from the top of the Lower,
through the passage-beds, and all through the Upper Tremadoe into
the Arenig. Olenus impar adds another to the characteristic species
of the Upper Tremadoc; and Cyrtoceras precox, which occurs at
Llanerch, is the earhest knewn Cephalopod in the British rocks.
The first Orthoceras (O. sericeum) known* also occurs in the passage-
beds at Garth and Tuhwnt-yr-bwlch.
It is clear that there is no stratigraphical or paleontological
break between the Lingula-flags and the Tremadoc: both areas
prove the former by direct evidence; and 9 species connect them
paleontologically, viz. Dictyonema sociale, Salt., Agnostus princeps,
Salt.. Ampyw prenuntius, Salt., Conocoryphe depressa, Salt., ? Olenus
ampar, Salt., Lingulellu Davis, M‘Coy, L. lepis, Salt., Obolella sagit-
talis?, Salt., Orthis lentrcularis, Wahl. Three of these same species
also connect the Tremadoe and Arenig: they are Lingulella Da-
visit, L. lepis, and Orthis lenticularis. All paleeontological evidence
goes to prove “ that the Tremadoc rocks of the St.-David’s area are
closely allied to, if not identical with, the lower portion of the
* Originally in the cabinet of Mr. D. Homfray, of Portmadoc,
g2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Tremadoc rocks of North Wales.” Mr. Homfray, of Portmadoe, than
whom no one has had greater experience or more carefully studied
the Tremadoc rocks in their original localities, finds no difficulty in
recognizing and correlating the rocks and fossils of the two districts,
affirming the St.-David’s beds to be the equivalents of the lower
portion of the series in the Portmadoc region. Mr. Homfray is
also of opinion that the Upper Tremadoc rocks are represented at
St. David’s by part of the Arenigs, which contain several Upper-
Tremadoce fossils, in addition to the rich fauna of Graptolites (42
species) now known to occur through the entire Arenig series.
The whole Tremadoc fauna consists of 33 genera and 86 species,
and no Hydrozoa; the Arenig includes 62 genera and 149 species,
with 42 species of Hydrozoa; the succeeding Llandeilo has 230
species, 90 of which are also Hydrozoa; yet in each formation the
Graptolites appear mostly to be of distinct species. They also play
an important part in the faunas of the Llandeilo, Caradoc, and
Llandovery rocks of Scotland.
Table VII. (p. t00) is a complete numerical analysis of the
fossils in the Lower Cambrian rocks, from the Harlech and Long-
mynd to the close of the Upper Tremadoc, in which it will be seen
that the twelve classes (and Plante?) are represented by 61 genera
and 182 species, as the known commencement of life in the British
area. They are as follows :—
The Longmynd group contains 18 genera and 33 known species.
The Menevian _,, - 24 5 Sy Ba a
The Lower Lingula-flags ,, 19 Bs SS) hie P
ThevWippers. 7s, va moae 12 45 AQ Fie be
The Lower Tremadoc _,, 26 . 515 Na Were “1
The Upper * # 21 $3 34 Ci, an
11 genera and 16 species pass to the Arenig, this small number
clearly determining the individuality of the Lower Cambrian fauna.
It is only through the 6 species of Crustacea out of 103, and the
6 Brachiopoda out of 20, that the passage-forms are thus numerous.
The remaining 3 species are pelagic, 1 Pteropod, 1 Heteropod, and
1 Cephalopod.
Lower TREMADOC.
Pranrxz.—None. ProtozoA.—None known.
Hyprozoa.— Dr. Callaway discovered in the Shineton Tremadoe
rocks two species previously unknown. One belongs to the genus
Clonograptus of Hall; the other is the Bryograptus Callavei of
Lapworth, both belonging to the family Dichograptidee. These are
the oldest Rhabdophora known.
Actinozoa.—None, so far as we know, below the Llandeilo rocks. |
EcHINODERMATA. Wind ocrinus Hann ensis, Hicks, and Paleaste-
rina ramseyensis, Hicks, are both from the Lower Tremadoc beds
of Ramsey Island, St. David's ; they are the first known species of
the orders Crinoidea and Asteroidea; and they stand with numerous
other discoveries as a testimony of the value of the researches of
Dr. Hicks in these early Cambrian rocks, to which Palzeozoic palee-
ontology owes so much.
ANNELIDA.—None, either in the rocks of South or North Wales.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 93
Crustacea.—Only 2 new genera appear with the coming-in of
the Lower Tremadoe (Psilocephalus and Neseuretus); but the whole
Crustacean fauna comprises 13 genera and 24 species, of which 10
genera and 19 species especially characterize the Lower Tremadoc.
They are so essential to a right understanding of the Lower Tremadoc
rocks and their entire distinctness from the Upper Lingula-flags that
tT enumerate them :—Agnostus Barlowu, Belt; A. dua, Call. ; Cono-
phrys salopiensis, Call.; Asaphus Croft, Call.; Diomde atra, Salt. ;
Lichapyge cuspidata, Call. ; Neseuretus (5 species, all by Dr. Hicks) ;
Niobe Homfray?, Salt.; N.menaprensis, Hicks; NV. solvensis, Hicks ;
Conocoryphe verisimilis, Sait.; Olenus triarthrus, Call.; O. Salter,
Call. ; Psilocephalus inflatus, Hicks ; and P. ennotatus, Salt. None of
the above species occurs below or above the Lower Tremadoc horizon.
The remaining five occur also in the Upper Lingula-flags, and unite the
two formations. The chief species named occur at Penmorfa, Borth-
wood, and Llanerch in Caernarvonshire, and Dudreath and Tyn-y-
ilan in Merioneth; and the same species occur in the St.-David’s
promontory at Whitesand Bay, &c. Nowhere do the species above
mentioned transgress the lower beds; the Lower and Upper Tre-
madoc are connected only by Agnosius princeps, Ampyx preenun-
tius, and Ogyqua scutatriv. Nothing that I could adduce would be
stronger evidence of the value of the Lower Tremadoc as a well-
defined zoological group: it contains more genera than any other
division of the Lower Cambrian stages ; and the species are essen-
tially characteristic.
Bryozoa.—Dictyonema sociale, Salt., as in the Upper Lingula-
flags. This genus occurs near Tremadoc in the passage-beds.
Bracutopopa.—The Lower Tremadoc Brachiopoda are Kutorgina
emgulata, Lingula petalon, Lingulella Nicholson, L. lepis, Obolella
Beltu, O. sabrine, O. plicata, and O. sagittalis. Orthis carausit,
O. lentecularis, and O. menapie. 4 of these 5 genera and 6 of the
11 species pass to the Upper Tremadoc. ‘They are Lingula petalon,
Lingulella lepis, Obolella Belin, O. plicata, Orthis carausw, and
O. lenticularis. 4 genera and 5 species appear from the Upper Lin-
gula flags, so that the true Lower Tremadoc species are few, and only
2 species are peculiar, viz. Lingulella Nicholsont and Opolella sabrine.
LaMeELLiBRANcHIATA.—The first appearance of this class, or the
earliest known in the British rocks. Dr. Hicks, through his
researches upon the Tremadoc rocks of Ramsey Island, has obtained
these first evidences of Pelecypod or bivalve molluscan life. He
refers them (and, I think, rightly) to 5 genera and 12 species—
Dandia (2), Glyptarca (2), Modiolopsis (4), Palearca (2), and
Cicenodonta (2); none of the species is known out of or above
the Lower Tremadoc.
GastERoPpopA.—None known below the Arenig rocks.
PrEeropopa.—The genus Theca is represented by 5 species in the
Lower Tremadoe, viz. Theca ovata, Salt., T. bijugosa, Salt., 7. cuspi-
data, T. Davisw, and T. (Cleidotheca) operculata. The 3 first
named pass to the Upper Tremadoc. 7. Davisz is the only species
in the Tremadoe rocks of St. David’s. The remaining 4 are North-
Welsh Tremadoc species.
94. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Herrroropa.—bellerophon ramseyensis, Hicks, B. solvensis, Hicks,
and B. shinetonensis, Call. ; the former both Menapian forms, cha-
racterizing the Tremanhire or Solva and Ramsey-Island beds, St.
David's.
Crpnatopopa.—None below the Upper Tremadoc.
The analytical Table No. V. shows that 28 genera and 58 species
occur in the Lower Tremadoc beds of North and South Wales. Three
classes only are of numerical importance :—the Crustacea with 13
genera and 24 species: the Brachiopoda, with 5 genera and 11
species; the Lamellibranchiata, 5 genera and 12 species. These
3 groups constitute the mass of the known genera and species, or
23 out of 29 genera and 47 out of 59 species.
Taste V.—Lower Tremadoe.
ee rom Pass to
Uopes Cl Genera. | Species. | Uppe
Lingula- asses, enera. | Species. | Upper
flags. Tremadoc.
| Plante.
Protozoa.
Hydrozoa.
Actinozoa.
Hehinodermata...... 2 2 |
Annelida..,
5 Crustacea) Wi... sas: 18 24 x
i Bryozoa. if 1
3 Brachiopoda ......... 5 ll 4
Lamellibranchiata... +5) 12
Gasteropoda.
Pieropoda: fs... 1 5 x
Heteropoda ......... I 3
| Cephalopoda.
WT Meecéusbhooacoon 28 58 8
Uprer Tremapoc.
Praniva.—None.
Prorozoa.—None.
Hyprozoa.—None.
EcuinopERMATA.—None.
ANNELIDA.—Tracks only.
Crusracra.—1l1 genera and 15 species constitute the Crusta-
cean fauna of the Upper Tremadoc; 12 of the 15 species are Tri-
lobita ; the remaining 3, Ceratiocaris (2 species) and Lingulocaris,
are Phyllopoda, and the first of this order known in the British rocks.
Asaphus affinis, M‘Coy, A. Homfrayi, Salt.,Cheirurus Frederici, Salt.,
Dionide atra, Salt., Ogygia scutatria, Salt., and O. Selwyni, Salt.,
pass to the Arenig, and, with 6 Brachiopoda and 3 Pteropoda,
constitute the 13 uniting forms out of a total of 182 species in the
Lower Cambrian rocks and 150 in the Arenig.
The following 5 Crustacea only are confined to the Upper Tremadoe
— Angelina Sedgwickii, Conocoryphe olenoides, Olenus ampar, Ceratio-
ris laius, and Lingulocaris lingulocomes. Lam careful to name these
ANNIVERSARY ADDRESS OF THE PRESIDENT. 95
as the first zoological or paleontological break between the Lower and
Upper Cambrian, or the Cambrian and Silurian, takes place here,
and that without any stratigraphical or physical ‘unconformity. No
greater faunal change is known to take place through the whole of
the Paleozoic rocks than at the close of the Tremadoc or Lower
Cambrian.
Bryozoa.—None known.
Bracutorpopa.—Only 4 genera and 7 species occur ; and 6 of these
pass to the Arenig. ‘They have therefore no stratigraphical value.
Obolella Belti is the single remaining or restricted form.
LAMELLIBRANCHIATA.—None yet known.
GastrRopopA.—None have yet occurred below the Arenig.
Prerovopa.—Conularia and Theca—the first with 1 species, C.
Homfray?, which is also Arenig ; the latter contains 6, one of which
(Theca simplex) also passes to the Arenig.
HerEeropopa.— Bellerophon arfonensis, Salt., and B. muliistriatus,
Salt., are the only Upper-Iremadoc species. The last-named spe-
cies is Arenig also.
CupHaLopopa.—Cyrtoceras precox, Salt., and Orthoceras sericeum,
Salt.; the last also passes to the Arenig; they are the first Cephalo-
pods known ; and it is doubtful if Cyrtoceras precox is not Lower
Tremadoc also. The rich locality Garth yields O. sericewm from the
upper part of the Upper Tremadoc. The Arenig of Llanvirn at
St. David’s has yielded the same; it is therefore both a North-
and South-Wales species, from the Tremadoc in one area, the Arenig
in the other.
TasLe VI.— Upper Tremadoc.
From
Lower Classes. Genera. | Species.
Tremadoc.
———— | |
Plante.
Pass to
Arenig.
Protozoa.
Hydrozoa.
Actinozoa.
Echinodermata.
Annelida.
‘| Crustacea ....ss..06+- ll 15
|
|
Bryozoa.
Pe
uN
J
op
Brachiopoda .........
Lamellibranchiata.
Gasteropoda.
Pheropods -2203.... 52: 2 C
Qe
Heteropoda ........ e 1
Cephalopoda......... 2
96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Description of the first six Tables.
I have in this oldest Cambrian series (from the Longmynd rocks
to the Upper Tremadoc) given an analytical table for each of the
6 formations or groups of strata. They cannot be otherwise tho-
roughly comprehended, taken as a whole, without wearisome de-
scription, owing to the non-representation of some classes, and -
the unequal representation and distribution of others. Neverthe-
less I have constructed Table No. VII. for the whole, to show
the unequal distribution, the Table delineates every thing, its
accuracy being tested through the six smaller tables (Nos. I. to
VI.), wherein are given the analyses of all the groups sepa-
rately. More than this, these six small tables enable the student
to see immediately the numerical value of each division, and the
number of species that pass up or live on to the succeeding period
or formation. Again, there is much difficulty in following some
authors through the many subdivisions and local names adopted by
them for the strata between the Longmynd group and the close
of the Upper Tremadoc. The succeeding Arenig, in which some of
the classes are largely represented, while the formation is widely dif-
fused geographically, enables me to show the distribution in one
Table (No. VIII.); the same is also done for every succeeding epoch.
Tur Lonemynp anp Hartecs Grovrs.—Table I. enumerates
the fauna of the Longmynd and Harlech beds only, chiefly those
of St. David’s, and the first traces of life in the British Islands.
In this Table 8 if not 9 of the 14 classes have no representa-—
tives, no species of them having as yet occurred; and, with the
exception of the Crustacea, the remaining 5 classes are but feebly
illustrated. This Table, however, at once lays bare the fact that we
are not tabulating the commencement of life even in our own area;
both the rock masses and the fossils that do occur, notably the great
Paradoxides, bid us search still deeper in time for their ancestors as
well as those of the pelagic Mollusca, as also of the Brachiopoda
(Lingule, Obolelle, and others). All these and the Lyssakine hexac-
tinellid sponges had their progenitors, which we have yet to deter-
mine. I doubt not that much light will yet be thrown upon them.
through patient research.
This first Table shows that the Longmynd and Harlech rocks are
known at the present time to possess 18 genera and 33 species—-
the commencement of life, so far as we know. The Crustacea are
the most abundant class; 7 genera and 14 species occur: these
earliest rocks of St. David’s yield Agnostus cambrensis, Hicks,
Conocoryphe bufo, Hicks, C. Lyellii, Hicks, C. solvensis, Hicks,
Microdiscus sculptus, Hicks, Paradowides aurora, Salt., P. Hicksi,
Salt., P. Harknessti, Hicks, P. solvensis, Hicks, MS., Plutonia Sedq-
wickii, Hicks, and the Longmynd form Paleopyge Ramsayii, Salt. ;
the Ostracoda are Leperditia ferruginea, L. cambrensis, Hicks, and
L. primeva. 4 of the above species pass to the Menevian—Agnostus
cambrensis, Conocoryphe bufo, Paradoxides aurora, and P. Hacksu.
Out of the 6 species of Brachiopoda, 4 also pass to the Menevian—
ANNIVERSARY ADDRESS OF THE PRESIDENT. 97
Lingulella ferruginea, Salt., and var. ovalis, Hicks, Orthis sagittalis,
and Discina pileolus. The special or restricted forms are only 2—
Discina caerfaiensis, Hicks, MS., and Lingulella primeva, Hicks.
The Plantz ? and Protozoa are mentioned under those heads in the
analysis. The table shows that 8 out of the 14 classes are not repre-
sented in the Harlech group. That they will remain so under re-
newed search and scrutiny I much doubt. Hach year adds some
new form to these once believed to be unfossiliferous strata. North
Wales has yet to yield up from these rocks a fauna equal to that
of South Wales.
Menevian.—Table IT. gives us all that is known of the Menevian
fauna and its relation to the Harlech series and the succeeding
Lower Lingula-flags, of which, indeed, it is but the base; for out
of the 24 genera and 51 species in the Mevevian, 13 of the former
and 19 of the latter are common to the two. Of the Crustacea 8 of
the 12 known genera, including 14 species, are the same—viz.
Agnostus (A. Davidis, A. scutahs), Anopolenus (A. Henrici, A. Sal-
teri), Conocoryphe (C. applanata, C. humerosa, C. variolaris), Holo-
cephalina (H. primordialis), Leperditia (L. Hicksir), Primitia (P.
solvensis), Microdiscus (M. punctatus), Paradowides (P. aurora,
P. Davidis, and P. Hicksu); and 3 of the 4 genera of Brachiopoda,
Lingulella (L. ferruginea), Obolella (O. maculata), and Orthis (O.
sagittalis). Of the 6 species of Pteropoda, only 1 is common to the
2 groups, namely Theca corrugata. The Menevian is united to
the Harlech and Longmynd rocks through 8 genera and 12 species.
The Crustacea by 3 genera with 4 species, viz. Agnostus (cam-
brensis), Conocoryphe (bufo), Paradoxes (P. aurora and P. Hicksir) ;
and the Brachiopoda the same, Discina (pileolus), Lingulella ( fer-
ruginea and var. ovalis), and Orthis (sagittalis). The Lyssakine
sponge (Protospongia) and Theca penultima complete the alliance.
- 8 of the 14 classes are not represented. The first Cystidean,
Protocystites menevensis, Hicks, occurs in the Meneyians of St. David’s.
11 new genera (not known in the Harlech group) first occurred in
the Meneyian sea ; 6 are Crustacea, 2 Pteropoda, 1 Cystidean, 1 An-
nelide, and 1 Brachiopod? No species pass from the Menevian to
the Middle or Upper Lingula-flags.
Lower Lineuna-riaes.—Table III. But for the Crustacea, the
Lower Lingula-flags would have no value as a subformation ; they
are but the upper, continuous development of the Menevian. Only
one genus of Crustacea, the Phyllopod Hymenocaris, is new to the
Lower Lingula-flags ; the remaining 8 are also Menevian; and 14 of
the 25 crustacean species also occur in the Meneyian below. Still
further, of the 17 known Lower Lingula-flag genera, 13 are Mene-
vian ; and this close association is more marked still from the fact
that only 2 species pass to the Middle and 8 to the Upper Lingula-
beds; so that there is a greater difference between the Lower and
Upper Lingula-beds themselves than between the former and the
underlying Menevian. The Upper Lingula-flags, through their
Crustacea, 8 genera and 30 species, stand alone.
Urrrr Linevra-riacs.—Table LV. Out of a community of 17
98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
genera and 36 species in the Lower, and 16 genera and 41 species in
the Upper Lingula-fiags, only 8 genera and 8 species unite the two
groups: they are 5 Trilobita and 3 Brachiopoda—namely Anopolenus
Saltert, Hicks, Microdzscus punctatus, Salt., Agnostus princeps, Salt.,
Paradoaides Hicksir, Salt., P. aurora, Salt., Lingulella Davisii, L.
lepis, and Orthis sagzitalis. Only 4 classes are represented in the
Upper Lingula-flags, the Annelida, Crustacea, Bryozoa, and Brachio-
poda. The remaining 10 have no representative whatever. 16
genera and 41 species occur in the Upper Lingula-beds ; 8 genera and
30 species are Crustacea, and 5 genera and 8 species Brachiopoda ;
there are 2 Annelida, and 1 Bryozoon, Dictyonema. 9 genera and
10 species pass to the Lower Tremadoc.
Lower Tremapoc.—Table V. The Lower Tremadoc fauna nume-
rically consists of 28 genera and 58 species; and the fauna is
compact and characteristic. Only 8 genera and 9 species appear
from the Upper Lingula-flags below: 4 of them are Crustacea; and
5 are Brachiopoda, and, with Dictyonema, complete the incoming
species. The one remarkable feature in the group is the presence
and first appearance of 5 genera and 12 species of Lamellibranchiata.
Dr. Hicks discovered them in the Upper Tremadoe beds on Ramsey
Island. They mark an epoch in the history of the class. Davidia
and Glyptarca are new genera, Modiolopsis, Palearca, and Cteno-
donta receive Mr. Hicks’s 8 other species. Until this class is
found in lower beds, these 12 species identify the Lower Tre-
madoc of Ramsey Island as an important horizon in time and space.
Only 4 of the 13 genera and 4 of the 24 species of Crustacea pass
to the Upper Tremadoc; they are Agnostus princeps, Ampyaw pre-
nuntius, Olenus alatus, and Dikelocephalus furea ; and 4 genera and
6 of the 12 species of Brachiopoda also connect the Upper with
the Lower Tremadoc; they comprise the following—Lingula pe-
talon, Lingulella lepis, Obolella Belti, O. plicata, Orthis Carausii,
and O. lenticularis. These and Theca ovata, T’. bejugosa, and T. cus-
pidata, in all 9 genera and 13 species, constitute the transgressing
fauna.
Urrrr Tremapoc.—Table VI. Nine whole classes are wanting
in this uppermost division of the Lower Cambrian rocks. Only 20
genera and 33 species compose the fauna of the Upper Tremadoe.
We have seen that 9 genera and 13 species pass from the Lower Tre-
madoe, thus leaving only 11 genera and 20 species as truly belong-
ing to the Upper Tremadoc. More than 50 per cent. of the species
pass to the Arenig, or 11 genera and 16 species. These few species
little affect the question of the paleontological break that takes
place here ; for 42 new genera and 133 new species make their ap-
pearance in the succeeding Arenig, through some physical changes
accompanying the zoological, which we have not yet been able to
satisfactorily discover. Unconformity between this group and the
Arenig is not known in the typical areas of South and North Wales;
but at no time in the history of the lowest Paleozoic rocks has appa-
rent extinction on the one hand, and migration from some unknown
area in the other, taken place so markedly. We have yet to learn or
ANNIVERSARY ADDRESS OF THE PRESIDENT. 99
trace whence came for the first time the 17 genera of Hydrozoa, the
17 genera of Crustacea, 5 Annelida, 3 genera of Brachiopoda, and 5
of other Mollusca, &c., all presenting a different facies, or an aspect
having little affinity with the previously existing fauna. The advent of
the 17 genera and 42 species of Hydrozoa and the 35 species of Crus-
tacea, all new forms and widely spread, has still to be explained.
The 13 species connecting the Upper Tremadoc with the Arenig
belong chiefly to the Crustacea and Brachiopoda, these two classes
yielding 13 out of the 16 species. The 6 Crustacea are Asaphus
affimis, M‘Coy, A. Homfray2, Salt., Checrurus Frederici, Salt., Dionide
atra, Salt., Ogygua, scutatria, Salt., and O. Selwyni, Salt.; and the
Brachiopoda, Lingula petalon, Hicks, Lingulella Davisti, M‘Coy, L.
lepis, Salt., Obolella plicata, Hicks, Orthis Carausit (Hicks), and
O. lenticularis. With these are Theca simplex, Salt., Conularia
Homfrayt, Salt., and Bellerophon multistriatus, Salt.
The Table numbered VII. embraces or shows the numerical value
and stratigraphical distribution of the species through all the Lower
Cambrian divisions, or from the Longmynd and Harlech group to
the close of the Tremadoe, and also shows in the last column, headed
“‘ Pass to Arenig,” the number of species that pass to that forma-
tion, or the base of the Silurian as now recognized by many syste-
matists. It will be seen that 11 genera and 16 species (14) pass
to the Arenig ; and this mode of expressing the connexion between
the lower and succeeding formations is carried through all the
Tables. Thus the right-hand column shows the number of species
passing up to the succeeding formation, and the left-hand column
(in all the Tables but this) those that came from an older or lower
series. As this special Table, and also Table No. I., shows the
commencement of life in the lowest rocks of the British Islands,
there are no forms older than those expressed by the number 61 genera
and 182 species. Their ancestors we know not; neither do we
know whence was derived the fauna given under the 11 classes. The
6 smaller Tables distinctly show the more immediate relation of the
several divisions of the Lower Cambrian rocks: nevertheless this
completer Table is of value, showing, as it does, the whole range
from the Longmynd rocks to the top of the Tremadoe.
I have endeavoured in my analysis of this Table, as in all the
subsequent ones, to express in words the result of the figures,
without which the Tables would merely enumerate the facts of
occurrences of no value to the student of geology and paleontology ;
and although of necessity tautology must be frequent, yet the
explanation, it is believed, will be clear. Throughout the whole
of the Tables (and there is one for each epoch) the genera
and species are given in the simplest form—the upper ficure
in each square (and under each formation) enumerating the num-
ber of genera in the respective horizons, and the lower figure
4 genera
20 species *
gives the census both zoologically and stratigraphically ; z.¢. there are
4 genera and 20 species in the given horizon or formation. In this
demonstrating the number of species, thus : This at once
I0o PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Table or record of the earliest rocks known, the numerous blanks
show that the classes were not represented or had not appeared
in the British Isles; but as we proceed through the formations we
find that in time, or as life progresses, all the classes become repre-
sented. The study of these Tables with the description may be
useful ; and it is hoped they will be found not far from the truth,
and exhibit the present state of our knowledge of the British species
and their distribution in time.
Taste VII.
| , 1
5 eS
B Sas
Shee | iso |a
= g cI or al 3 ws
Classes. é -| BR] 8 AA Sasi. &
: 8 ES la 2la Blade, 25) 5
5 | +3 5 6 la Sz Giesjasle3
2) 8/8) 8 (6h em|6 A Bale &
SGlalH|/a HH P HH Pp [AS
ee SSS ania maa >
Plambee ese. ee ceceivwcsee 2d
Protozoal .m.h-secmer.<oek bod g.tde tie | z
Actinozoa.
Echinodermata......... 33s hace Jel oodadl eet 4 odode | eee =
{
AMMEN Ga, 2 eeancs edoosaces STP Oe gS oll Rani s
|
Crustacea, .....2.-..-<.28| 20 (03 47, || 2 al eae alist eben teen ie
BLyOZOARe eee ee sees Dy reel erases emcee leeeoee} 2 [7
Brachiopoda ............ 54 20 bs Soh See eC
Lamellibranchiata ...| 5 | 12 }...... sere grease lasode ae
Gasteropoda.
! |
Pheropodai 2.5. wacmeems- lds || gsc toa Be leer 2 : :
Heteropoda lesdce.cee Na aa ol ers | “aliod| a deeaal eed 2h Leweilegaa
Cephalopoda ............ FV lees liceeosd|2s.i00¢ [ctw tone 2 ee
ee ere es eoumee Peer Ee
2 8S | 24 17 16 28 20 14
61 182 3 besa 36 Al 58 33 16 |
Arentce Rocks.
The Arenig or Skiddaw group of Sedgwick, immediately under-
lying the Llandeilo flags, forms the base of the true Silurian rocks.
From Arenig-fawr Prof. Sedgwick and Mr. Salter obtained two of
the characteristic fossils, Calymene parvifrons and Ogygia Selwyni.
Sedgewick recognized these beds as being different from the Llandeilo
above, and called them Arenig slates, believing them at the time to
be the top of his Ffestiniog group. The group is distinctly recog-
nized in the lead-mining district of the Stiperstones area, east of
the Longmynd, underlying the true Llandeilo flags of Shelve and
Corndon Hill, the Lower Llandeilo of Murchison. Salter first recog-
nized the Arenig group near St. David’s, passing upwards into the
Llandeilo flags, which are so finely shown at Abereiddy Bay. The
ANNIVERSARY ADDRESS OF THE PRESIDENT. IOI
distinctness of the Arenig from the succeeding Llandeilo is clear,
both physically and palzontologically. The following table exhibits
most of the type forms occurring in the Arenig and the Llandeilo :—
Lower
Llandeilo.
Upper
landeilo.
Ir
|
|
BPI CMAGAL 6.4 2c .eecescianesie ads x |... | ... | St. David’s, Whitesand Bay.
SELLA 1 ee x |... | ... | Stiperstones and N. Wales.
Tai-hirion,near Arenig-fawr,
Shropshire.
Calymene parvifrons .........46. Mull ossejareo {
Afgiina binodosa ..............006- *
——— PTANIS ...........2ceceeeeeeees %
—— caliginosa.................000 *
Trinucleus Murchisoni ......... Koh assed eee { Pee Ae teams (1S
stones).
(EULTLDSTT. | Seo ets eee x |... | ... | .Whitesand Bay.
Orthoceras Avelinii ............... * |... |... | Stiperstones.
Obolella plumbea .........s0...-... * | x2 | x 5
Cucullella anglica ..........0.... oe ha | eee 5
IBICRIMIGCS CSD: 5. .s-s-0-2ceceeees *
Asaphus tyrannus...............06.
POCA SKCS Ps caiiowiones'sincsonee -
Ogygia Buchii, var. convexa ...
Calymene cambrensis ............
SRPIMWELCHS LAVUS® ..........0...00 06
Lichas patriarchus ...............
Bellerophon bilobatus ............
EUCHECO FOUR was i... van caessneeen se
iimeulaeranulata ..............-
AELCWMALA wos... sescccececcceee
Orthisctriatula.... 0s. 6.
GnllioramMa .2.%-.4.0s.00:
Crenadonta,.? Sp. ...05.0...00-s00 abe
*
x
| Rrenyn in L. Llandeilo.
*K OK
Fairfach, near Llandeilo.
* OK 2K OK OK
KOK OK OK
Gilwern, near Builth.
Ogygia (Asaphus) corndensis ..
il Abereiddy Bay.
15-716 ST Re cs ae
Barrandia (Ogygia) radians ...
(COR LPI Cae ate eee eee
Calymene duplicata ...............
Trinucleus fimbriatus ............
Cheirurus Sedgwickii ............
PANE MUMANIS © oo... 60.2... .ceeeseees
Aenostus Maccoyi °...........:...
Lingula Ramsayi ..................
Bellerophon perturbatus .........
Murchisonia simplex ............
Modiolopsis inflata ...............
Didymograptus Murchisoni ...
@rthis calligramma ...............
*«
1k
Builth and Abereiddy Bay.
*K kK OOK xk OK
—-——4-
Abereiddy.
KK Kok
Builth.
* kK OK
12 | 14?) 16
«The great break in organic life between the Tremadoc slates
and the Arenig or Skiddaw group determined Salter, after working
VoL. XXXVII. 4
I02 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
out the two faune in the Tremadoc area in 1853, to regard the
Arenig as the base of the Upper Cambrian of Sedgwick” *. Phillips
regarded the Arenig as the upper or terminal member of the Middle
Cambrian. Upon fossil evidence we may commence the Upper
Cambrian of Sedgwick with the Arenig series, which is represented
in the ‘“Stiperstones” district. It was not until 1859 that Mur-
chison and Salter described the fossils of that area, although Sede-
wick in 1843 established the Arenig group, and subsequently
obtained the same fossils from the Skiddaw Slates, which were
described by M‘Coy previous to 1851. Salter, from the majority of
the fossils in the T'remadoc and Arenig groups, considered (and, I
believe, rightly) that the Tremadoe is the ‘natural termination ”
of the Ffestiniog or Middle Cambrian series, and the Arenig the
base of Sedgwick’s Upper Cambrian. Lyell adopted this view in his
manual; and Hicks and others have followed Salter in thus placing the
two groups. In the Cambridge Catalogue the Arenig is treated partly
as an intermediate group; and although it is 4000 or 5000 feet in
thickness, yet the number of known species is few—about 60, all
named, in the Woodwardian Catalogue. |
That there is a perfect, continuous, and conformable succession
from the Tremadoc into the Arenig rocks, admits of no doubt. It
is true that this is seldom seen, even in the areas where they are
typically developed. In the Shelve and Stiperstones districts, where
36 species are known, and in the Skiddaw area, yielding 76, no
downward stratigraphical succession has been truly or definitely de-
termined. The Arenigs seem to stand alone, especially in Westmore-
land, where no older stratified rocks occur with which to compare
them. In South Wales, however, at St. David’s, their base rests upon
the Tremadoc, and their summit is overlain by the Llandeilo beds of
Abereiddy Bay, both clearly defined. The three divisions here have
yielded no less than 96 species, 40 of which are Hydrozoa, and 31
Crustacea. Every Graptolite here makes its first appearance in
time ; none are known below the Arenig rocks. Six Crustacea out
of the 31 are derived from the Tremadoc, and only 3 pass to the
Llandeilo ; therefore 22 species are peculiar to the Arenig. Indeed,
out of the whole Areriig fauna, comprising 149 species, all but 38
are restricted to it. No more distinct group occurs in the British
Islands.
ArEnIG Rocks oF Norta WALES.
Professor Sedgwick, in 1852, described the Arenig slates and
porphyries of North Wales as forming a distinct and well-marked
subgroup in his previously named “ Ffestiniog group,” and as rest-
ing upon the underlying Tremadoc slate. It is also the “ great
eroup of roofing-slate and contemporaneous porphyry ” described ds
occurring in the chains of Arenig, Arran Mowddwy, and Cader Idris,
and in the Ffestiniog mountains, or the western base of the Arenigs
and Arran, and probably the Stiperstone rocks. For many years
* Catalogue of the Collection of Cambrian and Silurian Fossils in the Geolo-
gical Museum of the University of Cambridge, p. 18.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 103
the elucidation of the true position of the Arenig group in North
Wales remained a doubtful matter; probably the slates of Angers
are of the same age. Mr. Salter did much in 1853 to unravel the
structure of the Portmadoc area, and was enabled to correct the
nomenclature and distribution of the so-called Lower Llandeilo
rocks of the Penrhyn promontory, between Traeth-bach and Traeth-
mawr, and of the country to the east, towards the Arrans. The
succession across the Penrhyn promontory, from the Lingula-flags to
the Arenig beds, is complete ; and itis here that the Tremadoc slates
and Arenig beds are typically developed in North Wales, the close
of the Tremadoe and base of the Arenig being everywhere marked
by the presence of a well-defined band of “ grit,” varying in thick-
ness. ‘The position of this grit had long been fixed by the late Mr.
Salter in his Penrhyn section ; but it was left for Professor Ramsay,
in 1874, with Professor Hughes, Mr. Homfray, and myself, to trace
this zone from Ogof-dua, near Criccieth, to Drws-dwgoed, under
the Dolbenmain alluvium, and on to T'ai-hirion ; and in 1875 the late
Mr. Ward and Mr. Herbert continued and completed the survey of
it west of the Arenig and the Arrans on to Cader Idris, until last
seen passing under the sea at Towyn. This line is the base of
Sedgwick’s Arenig slates and porphyries, and of the great roofing-
slate series of the Ffestiniog area. Although occasionally obscured
by faults, it is never lost, and must be traced by all who would
understand the succession in North Wales between the Tremadoc and
Arenig series. The fossils, when seen, at once determine the posi-
tion—Psilocephalus innotatus, Niobe Homfrayi, Asaphus Homfrayt,
Lingulella Davisir, and Dictyonema sociale illustrating the lower part
of the Tremadoce, and Angelina Sedqwicku, Asaphus Homfrayi, and
Ogygia scutairia at Garth and Penclogwyn the upper ; whereas, suc-
ceeding the grit-band above named, at Ty-obry, Tai-hirion, &c., Caly-
mene Murchisom, Asaphus affinis, Dionde atra, and Aiglina caliginosa
are the characteristic forms, being Arenig fossils. Only about 16
species connect the two groups. This physical line, when once deter-
mined, is a marked feature at the base of the Arenigs, dividing the
two formations. Beneath the grit at Garth Hill and Deudreath oceur
the upper beds of the Upper Tremadoe slates (hard grey flags), rich
in fossils, including Asaphus Homfrayi, Angelina Sedqwicku, Ogygia
scutatriv, Lingulocaris lingulecomes, Cheirurus Frederici, and Co-
nularia corvum. These hard grey beds at the top, some would
separate from the Tremadoc group, purely upon paleontological
grounds, or because certain species above named are common to the
two horizons. Some regard must, however, be paid to stratigra-
phical evidence.
There is no distinct passage-bed containing fossils between the
Upper Tremadoc and the Arenig. Through the Portmadoe district
the two groups are separated by a peculiar band of felspathic grit,
which intervenes to cut off the upper (volcanic) series from the true
Tremadoc slates below. ‘This felspathic grit, variously conditioned,
may be traced along Yr-allt-wen, above Tremadoc, and across the
estuary of Treath Maw; it constitutes the brow of the Garth, and
22
I04 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
ranges under the foot of Moelwyn to the Manod mountains on the
east. This zone, all along its course, indicates and ushers in a new
set of conditions, physical and paleontological. No Graptolites
occur below this line anywhere; but in the black slates immediately
overlying it at Garth &c. they occur in plenty, associated with cer-
tain species of Homalonotus, Asaphus, Calymene, Aiglina, and Dio-
nide, accompanied by Conularia and Lamellibranchs; and among the
lower beds of the volcanic rocks of the Manods Calymene parvifrons
and Trimucleus Murchisons occur, accompanied still further eastward
by Ogygia Selwynu, the species, of all others, which characterizes the
Arenig rocks of Shelve and Skiddaw, and occurs at Llanfaelrhys, in
South Caernarvonshire, associated with Lingula attenuata and Grap-
tolhithus Murchison. ‘This classification is borne out by the persis-
tent position of the grit which everywhere separates the two hori-
zons palezeontologically as well as stratigraphically, the mass of the
Arenig with its peculiar fauna not occurring until the grit is
passed. No species of Rhabdophora is known below this grit (their
first appearance being in the Arenig rocks); and although the
Arenig Graptolithide are rare in North Wales (4 species), as com-
pared with Skiddaw (27 species), or with South Wales, St. David’s.
(18 species), still the distinct Crustacea must be held as significant.
Again, comparing the value of the same formation in North and
South Wales, it is important to remember that, of the whole Arenig
fauna in South Wales (97 species), only 5 north-west forms are
common to the two areas: these are Calymene parvifrons, Ogygua
Selwynu, Aighna caliginosa, Lingulella Davis, and Orthis lenticu-
laris. 26 Trilobites, 8 Brachiopoda, 38 Rhabdophora, and 3 Ptero-
poda are peculiar and confined to South Wales. Thus amongst the
same group of rocks the correlation of species is a difficult question,
even over so small a geographical area as Wales. —
The dark slates at Ty-obry, which immediately overlie the grit,
contain Calymene parvifrons, diglhina caliginosa, and Diomde atra,
associated with Diplograptus mucronatus, Climacograptus confertus, —
and Gilossograptus ciliatus, all Lower-Arenig species. Palewarca
socialis and a species of Ctenodonta are the only North-Welsh
bivalves, and Conularia cortwm and C. margaritifera the only two
Arenig Pteropods known in North Wales. None of these occur in
the Arenig series of St. David’s, and none pass to the Llandeilo
group im any area.
The researches of Dr. Hicks at St. David’s have resulted in greatly
advancing our knowledge of Sedgwick’s group in that area*. In
his paper upon “the Succession of the Ancient Rocks of St. David’s,”
Dr. Hicks draws attention to the history of the names Arenig and
Llandeilo groups, and explains the manner in which the two series
were confounded by one of the authors who have written upon them,
and how the slates above and below the Arrans and Arenigs were
by him and the Geological Survey classed as equivalent to Llandeilo
flags of Builth &e.
The St.-David’s Arenigs consist mostly of black slates, resting
* Quart. Journ. Geol. Soc. vol. xxxi. pp. 167-194.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 105
conformably upon the Tremadoe group on the N. and N.E. side of
the anticlinal, and they may be continuously traced for many miles.
They occur also at Ramsey Island, and are there 4000 feet thick,
chiefly deep-sea deposits, and must have been of great duration, as
proved by their varied and distinct faunas.
Dr. Hicks divides the Arenig group, through its zonal contents,
into three subgroups, the Lower, Middle, and Upper Arenig. The
lower, or black slaty Arenig, strikes E.N.E. and W.S.W., and has
a vertical dip. The cliffs at Whitesand Bay and Road-uchaf, in
Ramsey Island, yield the chief fossils. Numerous species of Grap-
tolites have been obtained from this lower subgroup ; the Trilobites
Asaphus Homfrayi, and Ogygia scutatrix, with Conularia Homfrayt
and Lingulella Davisi, especially characterize this lower division, and
are associated with Phyllograptus stella, Trigonograptus ensiformis,
Callograptus radiatus, and Piilograptus Hicks. Dr. Hicks enume-
rates 25 species from this division, 28 from the middle, and 33 from
the upper*. Asaphus Homfrayi, Ogygia scutatrivc, and Conularia
Homfrayi are Upper-Tremadoc as well as Lower-Arenig forms, and
connect the two formations. I am not aware that Lingulelia Davisit
ever again appears above this horizon in the Cambro-Silurian rocks.
The middle slaty and flaggy groups are also best seen at Whitesand
Bay. In 1860 Mr. Gibbs, the late fossil-collector for the Survey,
obtained a few fossils here. The characteristic Trilobite Trinucleus
Gibbs was first obtained by him at Whitesand Bay, and subsequently
in the Skiddaw beds. This locality has furnished Ogygia bullina, O.
peliata, Aiglina grandis, Trinucleus Gibbsu, T. Sedqwicku, Ampyx
Saltert, Lingula petalon, and Orthoceras sericewm, with 6 genera and
11 species of Rhabdophora; all the above are essentially character-
istic of, and confined to the middle subdivision. Of the Graptolites
the chief are Tetragraptus crucifer, T. serra, T. Hicksu, T. Halli,
Clematograptus vinplicatus, Callograptus elegans, and C. Salterc.
Lithologically the Upper Arenigs resemble the Lower, being fine-
grained dark shales, 1500 feet thick ; they underlie the true Lower
Llandeilo near Abereiddy Bay, and are conspicuous for the new and
distinctive fauna and the first appearance of many genera of Trilo-
bites, distinctly marking a complete and progressive change from the
fauna of the Tremadoc below towards the introduction of succeeding
Llandeilo forms. Llanvirn quarry has yielded to Dr. Hicks a rich
group of species ‘distinct from any previously discovered in any
part of the Arenig series at St. David’s”?. Most of the genera are
new ; and several genera which appear for the first time, culminate
in the Llandeilo and Caradoc rocks; these are J//enus, Illenopsis,
Barrandia, and Phacops, each having a representative species, and
Placoparia, this last a genus new to Britain, hitherto only known in
France, Bohemia, and Spain. The occurrence here of this genus is
* These numbers are doubtless in excess;"many forms must give way on
eritical examination, numerous species being made upon fragments only.
Mr. Lapworth has already reduced them considerably. The Arenig of St.
David’s may yield 25 species; the whole Arenig probably about 50 species.
t Dr. Hicks, Quart. Journ. Geol. Soc. vol. xxxi. p. 174.
106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
important as bearing both upon distribution and correlation. Again,
the Gasteropoda first appear in Britain in the Upper Arenigs of St.
Dayid’s (Pleurotomaria llanvirnensis, and Ophileta or Raphistoma).
Yet, strangely, we have no record of any Lamellibranchs through
the whole of the Arenig group in South Wales; 4 species are known
from the Stiperstones area, and 2 from Ty-obry, in North Wales. It
will be remembered that no less than 12 species occur below in the
Lower Tremadoc rocks of the same area. The value of this upper
division of the Arenig group in South Wales is enhanced by its re-
semblance to Barrande’s Etage D1 (Bohemia), and its close relation
to the fauna found in the Arenig slates in North-west France. The
recognized presence of this stage in Britain enables us to correlate
our beds with those on the continent, and thus establish a general
succession for the Western-European and Western-British rocks of
this age.
This result is due to the researches of Dr. Hicks, as detailed in
his valuable papers upon the history and succession of the ancient
rocks of St. David’s. Carefully constructed tables, prepared for the
purpose of testing the value of the Arenig group and its relation to
the Tremadoc below and Llandeilo above, clearly show that it stands
almost alone ; for of the 55 known species of Hydrozoa in the Arenig,
only 2 species pass to the Llandeilo (Didymograptus Murchisont and
Climacograptus confertus). The first appearance and the abundance
of the Rhabdophora in the Arenig rocks would alone justify the posi-
tion now assigned to it as the base of the Lower Silurian rocks; only
1 species is known to occur in the Tremadoc group (Dendrograptus,
from the Shineton Shales of Shropshire). The crustacean fauna is
equally conclusive ; out of 50 Arenig forms known, only 2 (7rinu-
cleus Ramsayi, Hicks, and Homalonotus bisulcatus, Salt.) unite the
Arenig and Llandeilo through the Trilobita. Out of the 18 species
of Brachiopoda, only 3 pass to the Llandeilo, viz. Lingula brevis,
L. attenuata, and Orthis calligramma. No Lamellibranch, Pteropod,
Heteropod, Gasteropod. or Cephaloped (of which united, there are
30 species) passes to the Llandeilo. ‘Thus, out of the known fauna
of 149 species, only 16 pass upwards into or are common to the
Llandeilo beds. 150 species make up the entire known fauna of
the Arenigs; their distribution is as follows :—125 species occur
in the North and South Wales Arenigs, 34 from various localities
in North Wales (Tremadoc, Ty-obry, and Tai-hirion), and 94 in
South Wales; the Skiddaw species number 50 and the Stiper-
stones 36. ‘These two latter localities are important ; they are widely
separated, and very few species occur in common. Of the 50 Skid-
daw species of all classes, only 9 occur in the area west of the
Stiperstones in Shropshire ; this is due chiefly to the rich Grap-
tolite fauna, which group is largely represented, no less than 52
species occurring in the Skiddaw beds alone. West of the Stiper-
stones only 6 species are known; and they have an important bear-
ing upon distribution: they are Didymograptus patulus, Hall, D.
geminus, D, hirundo, D. constrictus, D. Murchisoni, and Clematograp-
tus implicatus. Diplograptus dentatus also occurs at Tremadoc and
ANNIVERSARY ADDRESS OF THE PRESIDENT. 107
Tai-hirion in North Wales, and ranges to both Llandeilo and Caradoc;
Didymograptus patulus, D. hirundo, and Clematograptus vmplicatus
are also present at St.-David’s*. Few Hydrozoa occur in the North-
Wales Arenigs; Ty-obry, Tremadoc, and Tai-hirion yield the few
that have been met with. 23 species range through the St.-Dayid’s
series, 2 of which only are common to the Stiperstones area, viz.
Didymograptus patulus and D. hirundo; and 5 or 6 ally them to
Skiddaw. There is thus little in common between the Arenigs of
Skiddaw and North Wales, few species connecting them. The rela-
tion, however, between the Skiddaw species and those of St. David’s
is closer, 5 or 6 being Graptolites, and 2 Trilobites (Ogygia Selwyni
and Trimucleus Gibbsiz). These, we must remember, are the two
largest groups, and have been most searched for, at St. David's
especially, by Dr. Hicks, and in the Skiddaw beds by Dr. A. Nichol-
son, Mr. Dover, and the Survey (through the late Mr. Ward).
The value of the Arenig group is still more apparent when we
consider the development of life that accompanied those physical
conditions and changes which took place at the close of the Lingula-
flag and Tremadoc epochs. We know that no less than 40 genera
make their first appearance in the Arenig rocks in the British Islands.
These 40 genera belong to the following 6 classes :-—
Hyprozoa 16: Callograptus, Dendrograptus, Phyllograptus, Di-
dymograptus, Azygoyraptus, Ptilograptus, Trigonograptus, Tetra-
graptus, Climacograptus, Nemagraptus, Dicellograptus, Clemato-
graptus, Diplograptus, Glossograptus, Dichograptus, and Logano-
graptus.
AnneLipa 4: Helmintholithes, Stellascolites, Nereites, and Palco-
chorda.
Crustacea 11: “glina, Trinucleus, Barrandia, Calymene, Pha-
cops, Placoparia, Illenus, Illenopsis, Homalonotus, Beyrichia, and
Caryocaris.
Bracuiopopa 2: Dinobolus and Siphonotreta.
LAMELLIBRANCHIATA 2: Ribeiria and Redonia.
GastERopops 3: Ophileta, Pleurotomaria, and Rhaphistoma.
The succeeding Llandeilo, as we shall see, was equally prolific, no
fewer than 48 new genera accompanying the complete change of
conditions at the close of the Arenigs and commencement of the
Llandeilo. This change was bridged over by orly 8 genera and 9
species passing to the Llandeilo in any area; 4 are Hydrozoa, 2
Crustacea (Zrinucleus Ramsay: and Homalonotus bisulcatus), 3 Bra-
chiopoda (Lingula brevis, L. petalon, and Orthis calligramma) ; and
only 3 range into the Caradoc. As before stated, the relation of
the Arenig to the Tremadoc is through 16 species, 6 of which are
Brachiopoda, 6 Crustacea, and 4 bivalve Mollusca. Thus 122
species out of 150 are strictly Arenig forms or confined to that
horizon.
* Five other Skiddaw species occur west of the Stiperstones, and, with the
6 Graptolites, tend to connect the Arenigs of Shropshire with those of West-
moreland. They are the Annelida Scolithus linearis, Salt., and Helmintholithus,
with Agnostus Moret, Salt., Ogygia Selwynit, Salt., and Zglina binodosa.
108 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Nothing can be more conclusive as to the value of the Arenig
group than the distinctive part played by its characteristic fauna
and its distinct stratigraphical position. Since the determina-
tion by Hicks of the St.-David’s fauna, Mr. Marr of Cambridge
recognized some fossiliferous shales south-east of Caernarvon, in |
three localities on the banks of the Sciont; these shales contain
Arenig species. The Trilobita and Brachiopoda indicate Arenig
affinities; and the Orthoceras caercesiense occurs only in the Arenigs
of Llanvirn, near St. David’s. The genus Caryocaris (a new spe-
cies of which has occurred here, C. Marri) hitherto has not occurred
out of the Skiddaw Slates of Cumberland (C. Wrightw being the
type). The associated Graptolites are those of the Skiddaw rocks
also, viz. Didymograptus bifidus, D. indentus, and the Llandeilo form
D. Murchison. The genus Barrandia would help to place these
beds either in the Arenig or the lower part of the Llandeilo group.
This locality is suggestive of the Arenig or Llandeilo beds striking
from Caernarvon to Bangor and Aber, west of the great fault that
runs from Dingle on the 8.W. to Aber on the N.E.
ARENIG oF SoutaH Wategs At St. Davip’s.
The following table enumerates all the species at present known
in the Arenig rocks of St. David’s ; it is convenient to subdivide the
group into 3 series, both on lithological and palecontological grounds.
It will be seen how distinct the fauna of each division or series ap-
pears. The total number of species at St. David’s is 70. The lower
Arenig has yielded 16 species, the middle 24, and the upper 33.
14 species are peculiar or confined to the lower series, 21 to the
middle, and 30 to the upper. No species out of the 70 occurs in all
three divisions. We thus see how distinctive a group of fossils
each subdivision contains. For the construction of the Arenig Table
(No. VIIL., p. 115) I have selected 18 localities from which the Arenig
species have been obtained, and tabulated 8 of the most important.
The four type areas, where the Arenig rocks are present and well
developed, are :—
1. Westmoreland: Skiddaw.
2. Shropshire: Shelve area.
3. North Wales: Tremadoe, Tai-hirion, &e.
4, South Wales: Ramsey Island and St.-David’s area.
The chief localities for fossils are the following 18, comprised in
the above 4 areas :—
1. Westmoreland: Skiddaw, Longside, Keswick, Outerside, Scaafel, White-
side, and Braithwaite River. 4
2. Shropshire: Shelve area (west of Stiperstones), Mytton Dingle, Perkins
Beech.
3. North Wales: Tremadoc, Garth, Ty-obry, Tai-hirion. é
4. South Wales: Ramsey Island, Llanvirn, Whitesand Bay, and St. David's.
ANNIVERSARY ADDRESS OF THE PRESIDENT.
Areng Species, St. David's.
109
Species. Lower. | Middle. | Upper.
RHABDOPHORA.
Didymograptus extensus, Hall ...............08 %
LETTE, ING Oe, WO anaes Ole pon eR ea eer au *
[SECIS 2 (01 Hoes DAM ee eee Re * *
bien ALOU T ees os title cakk schist oStiele tat mses’ *
PeMa GUUS PAU ess casaslectoeincie set eeee sess % x
BMAESUS, eLLODemewa. scene va dcticms cusstice've vide *
NOW CMEUS AONE ath... oe idvolaiicndasenessccs *
———INGCMOlsont, Lap .iscsecccesseseceeereeees: Ste *
Phyllograptus stella, Hall .......00....0ececeeseee *
PUI SIA Lice aeaica cto notiscleaie sSsiseaiscissebieis d's *
Trigonograptus truncatus, Lapw. .............4. %
emsionnis, Halles. .scasnssasesi cs sastae seeks *
eiostapuus EMCkKsi .2..5....2:20sstssacessea0s 0 *
Dicellograptus divaricatus, Hall ............... x
Diplograptus dentatus, Brongn...........0...066- *
Climacograptus confertus, Lapw. ............... See *
Clematograptus implicatus, Hopk. ............ *
Tetragraptus crucialis, Sal¢. ............0.0eee ee *
EINE O DICK Toes. 8 ote ae dun sin das ce saree cules x
LIP SIM OPK io loc Us wcnieavenedercscs senses %
eyouordes, PGI... c.%as.2esebasenses sce os *
quadribrachiatus, Hall ...........-.c.000--- %
SMTP OMG a. stun onus cee naduscees escac uses %
Glossograptus ciliatus, Hii.........cecseeeeeeeee *
CrusTACEA.
PSAnMISPELOMUPAYT, SALE. vo. lesnsienosccstt sense *
RTOS US MIUN GON SCUC.0 i cevsscsceesese-deeeesacc %
PAM SALCON, LLICKS oo nos cwevnascee MH acscene cast: *
PBeliMaeeRAMCIS, SAUL. 2... 0... cc ee sceesncsensceess %
LOT, JE GO AS BAS apee te ye SNC a eae Aer een at i *
Obtusicaudata, Aicks . 508... eels *
iBasranGtasclomibirayl, A2cks ...0...5..sene ase: *
Calymene Hopkinsoni, Hicks................0006+ *
PML OMS USOUG shee cach Geis ele soja esto ecco %
— Pyare MuUrchisoni Saleen a 43 %
», SID: Boot des Sak MANOR ae OSE eae oF nas Ace *
POEM BUSS i785 Cece Uh eek leldigoSae deta Mela kiele Hae *
Oevedarsemtatrix, SAC... s6c.cassncecssnescieetees *
MUG A ISL Ca, fo serivo ag Jgsesittic nnceearis ceeoe *
"DAW UTa Bis “PSYOMAES Meck Soares tem Soa Re a Rs *
Mlcemmomtughesti, AUCKS... fo .65.2.e6 le seveks cee: *
Illenopsis? acuticaudata, Hicks ............... *
Placoparia cambrensis, Hicks.............0.0+++0 af *
Phacops Ilanvirnensis, Hicks .........0..0..s0++: sie aN *%
Mrimteleus GalbDsit, SAC. ccoc.cc. ve sceseerecesneees *
Dem AWC KI WOR sno esate eaticscasenscacee *
EMCO COR, SOLE. « saceceues souls doudee soeedeees *
EVI SLY, MELICHSH. clic ccciseais aes décieleioa Rsv %
MSE Saisie Saisie oct aaa be cttasndasen aodeyiaes x
IE YNEIC NVA AB YDeg 7. 5 vsiae,s Seis siogin oataeleintininais som date te oiler *
Carried forward.....,...... 11 18 22
IIo PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Aremg Species, St. David’s (continued).
Species. Lower. | Middle. | Upper.
Brought forward) 11 18 22
BRACHIOPODA.
Lingulella Davisii, M‘Coy ........... Bor Nee erin *
Wine wlaypetalonne chs ene are ecm eee ere er % *
ingulayattenuata SOU: yeeeseene serene ecaeece 08 ea %
Discobolusv tacks eave nee eee eee *
DIS CIMAS SPE teste ie cia se oe Se an se icine rr wae %
Oris lenticularist)0l 7a ee ee earn *
iS Dus accilecceactcaseistrclmasct et cmamreec a tace ence at ve *
Ai) Ohne ars ie Seba Ue Tiel brane sneer a *
Obolellapplicata PECs aces eenesee ete eeeeent *
Siphonotmetayspycscaset ecco eee eeae eereea ter 60 %
GASTEROPODA.
Oplulletal spy. togs cs. cttbionecs wae toaenece toate 500 ane *
Pleurotomaria llanvirnensis, Hicks ...........- %
PTEROPODA.
Conularia dlonatraya Salt. scseeeee reset etceneee *
Manvatnensis" H7CS: ss aaeee ce oe ears *
Mhreca Cacreesiensisy ea7CHS 0% «cesacaeeee eee Bei bee *
lar knessil AICHhS cote te ce eh Renee fis %
HETEROPODA.
Bellerophon multistriatus, Salt. ............6.. siete *
=== AMVATTICNSISML CHS” a) Jneeceecoaeceeeence see ae *
CErPHALOPODA.
Orthoceras sericeum, Salt. ...::::.0.5..522c8sn.8ee a *
caereesiense, Wicks 2h. de ia, See ssc Bie %
ANNELIDA.
Buthotreplisisp.\.07lntecsesedsscece soccer sea e 400 Be *
16 24 30
The intimate stratigraphical conformity at St. David’s between
the Tremadoc and Arenig rocks, and between the latter and the
overlying Llandeilo series, is clear and determined, both on the
mainland and on Ramsey Island, where both the Tremadoc and the
Arenig occupy a considerable area. Much of the centre of the
island is composed of the Arenig series, and is prolific in fossils. The
slates of St. David’s are black and probably of deep-sea origin. The
subdivision here by Dr. Hicks into Lower, Middle, and Upper is
based upon the distribution of the organic remains and the relation
to the Llandeilo above. This comparison is important in its bear-
ing upon the value and meaning of the terms Arenig and Lower
Llandeilo as applied to at least four areas and groups of rocks in
England and Wales, viz.:—Westmoreland, or the Skiddaw group ;
Shropshire, or the Stiperstones series; North Wales, or the Tremadoce
and Ffestiniog areas; and South Wales, or the St.-David’s beds.
Formerly the Geological Survey regarded three of the groups in the
areas above mentioned as belonging to rocks termed Lower Llan-
deilo by Sir R. Murchison; they were mapped as Llandeilo simply,
ANNIVERSARY ADDRESS OF THE PRESIDENT. Ii!
the Survey not recognizing the two divisions termed Lower and Upper
on the maps, as they are not separable or distinguishable in the field
over large areas. The exact position of the Arenig group was, and
has for many years been, a doubtful question ; and it is due to the
continued researches of Messrs. Salter and Homfray in North Wales,
and of Dr. Hicks in South Wales, that the name and position assigned
to these beds by Prof. Sedgwick in 1843 is now revived and defi-
nitely established, and that the Arenig group of rocks and fossils
has now had assigned to it its true stratigraphical place above the
Tremadoe group and below the Llandeilo proper, and with a fauna
recognized as peculiarly its own. The Llandeilo of Murchison and
the Survey (first named in 1843) did not really include any of the
Arenig proper as determined in North Wales in 18438, 1846, and
1852, or as occurring in the chain of the Arrans, Arenig, Cader Idris,
and in the Ffestiniog region (typical districts). The term ‘‘ Lower
Llandeilo” of Murchison included Prof. Sedgwick’s “ Arenig,” not
as first intended ; and Prof. Ramsay, in the first edition of his ‘ Geo-
logy of North Wales’*, states that “since 1848 the Survey con-
sidered the slates close below and above the Arans and Arenigs as
equivalent to the Llandeilo fiags of Builth and Shelve” 7.
Mr. Salter, however, in the appendix to the same work in 1866,
pp. 293-257, under the section “‘ Lower Llandeilo” and plates 8-12,
clearly showed the importance of truly correlating the Arenig group,
eliminating it partly from the Upper Tremadoc below and from the
so-called Llandeilo above.
There is now no doubt whatever about the horizon or position
of the Arenig rocks. They are entirely distinct from the Tremadoc
eroup of Sedgwick, and were claimed as Lower Llandeilo by
Murchison. They are the “ Arenig and Skiddaw” group of Sedg-
wick, established by him in 1834, and confirmed through subse-
quent research in the Skiddaw area, and of which the fossils were
described by M‘Coy before 1851. Priority therefore under all heads
is due to the researches of Prof. Sedgwick. Finally Salter described
the majority of the fossils of both the Arenig and Tremadoc groups,
showing in the clearest manner that the Tremadoc rocks were the
natural termination of the Ffestiniog or ‘“‘ Middle Cambrian ” series,
and the Arenig group the base of the “Upper Cambrian” or
‘¢ Lower Silurian ” of Murchison ; these rocks through their fossils,
have their equivalents, as shown by Salter, in the Quebec group of
Canada.
Prantra.—None.
Prorozoa.—None.
Hyprqz0a.—Subsequent to the change of conditions which ter-
minated the Tremadoc period, or at the coming-in or commencement
of the Arenig deposits, no less than 18 genera and 42 species of
* Mem. Geol. Surv. of Great Brit. vol. ii. p. 6 (ed. 1, 1866).
t Sir R. Murchison, in 1834, termed the Llandeilo flags ‘“ Trilobite schists ”
in his description of the Shelve country, the Carneddau (Builth), and the
neighbourhood of Llandeilo; and under this name were included (near Shelve)
the strata as low as the base of the Stiperstones, the whole of these rocks being
older than the Caradoc sandstone.
I12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Hydrozoa first appeared in the British Arenig sea, and that with-
out any known previously-existing Ceelenterate fauna. We have no
clue to the area or region whence they migrated ; possibly Canada
may be selected as one, at least, of the probable areas for their
origin and dispersion. We regard the Quebec group of rocks as the
_ equivalent in time of our Arenig series; and they contain the same
species of Graptolites in great profusion. We cannot look to Scan-
dinavia for such an assemblage; and although the Bohemian Grap-
tolitic fauna was extensive, still, on the whole, I should regard the
Canadian, through certain genera and species, as being the source
of dispersion and migration. There is intimate agreement between
the faunas of many of the American and our own Paleozoic rocks ;
and this is notably the case with the Arenig and its Graptolites.
Thirteen genera and 28 species of Graptolites occur in the
Skiddaw group, showing that more than two thirds of the known
genera and species are in the almost barren slates of the Keswick
area; for, with the exception of 10 species of Annelida (all tracks
and burrows), 9 species of Crustacea, and 2 Brachiopoda, no
other forms are known—neither Lamellibranch, Gasteropod, Pte-
ropod, or Heteropod, so far as we know, ever having appeared
in the Skiddaw series west of the Stiperstones in the Shelve area*.
The Arenig rocks are there clearly exhibited, but yield only a
small series of Hydrozoa. Only 3 genera and 6 species have yet
been collected ; they are Diplograptus pristis?, Didymograptus pa-
tulus, D. geminus, D. hirundo?, D. constrictus, and Clematograptus
amplicatus. The Crustacea eminently characterize the Shelve
Arenigs; and it is through the 6 genera and 9 species of Trilobita
and the stratigraphical position that the age of the beds is clearly .
determined: 3 of the 7 genera that occur here are also in the Skid-
daw rocks—Agnostus Moret, Ogygia Selwynu, and Aiglina binodosa.
Next to North Wales the Shropshire Arenigs contain the smallest
number of species; but they are distinctively characteristic.
North Wales, from the Tremadoc and Ffestiniog areas at Tre-
madoe, Ty-obry and Tai-hirion, has yielded only 4 genera and 4
species.
: Next to the Skiddaw rocks and the Westmoreland area the chief
development of the Arenig group occurs in South Wales on the St.-
David’s promontory, at Llanvirn, Whitesand Bay, Trwyn-hwrd-
dyn, and Porth Melgan, and the rich locality of Ramsey Island.
These several localities have yielded, to the researches of Dr. Hicks,
Mr. Hopkinson, Mr. D. Homfray, and others, about 8 genera and
18 species of Graptolites. Only 3 species are common to North and
South Wales, namely Diplograptus dentatus?, Clumacograptus con-
fertus, and Glossograptus ciliatus ; 6 show the relation of the Skiddaw
rocks with South Wales, viz. Didymograptus affinis, D. brfidus, D.
patulus, Tetragraptus quadribrachiatus, Phyllograptus typus, and
Diplograptus dentatus?; and 7 are common to the Stiperstones area
and South Wales, viz. Didymograptus patulus, D. affinis, D. hirundo,
D. bifidus, Diplograptus dentatus, Clematograptus implicatus, and
* Lords Hill, Bog Mine, Dingle, Ritton Castle, Corndon, &e. .
ANNIVERSARY ADDRESS OF THE PRESIDENT. 113
Climacograptus confertus. Out of the entire fauna of the Arenig
Rhabdophora only 2 or 3 genera and species pass to the Llandeilo
rocks. ;
KcutnopErmMsta.—No record whatever of this class in the Arenig
rocks.
ANNELIDA.—The whole group, of which 9 genera and 11 species
are described, possesses no zoological value ; they are simply worm-
burrows, worm-tracks, or trails of Mollusca. Ten of the 11 so-called
Annelide species occur in the Skiddaw Slates, the one unrepresented
form being Buthotrephis from St. David’s. Scolithus linearis and
Helmintholithes are in the Stiperstone beds also. No species has
occurred in North Wales; and no species pass up from the Tremadoc
and Lingula-flags below.
Crustacea.—The Arenig rocks have unequally distributed through
them 14 genera of Trilobites and 48 species, Ostracoda 2 (Beyrichia
and Primitia) and the Phyllopod Caryocaris Wrightt increasing
the Crustacean fauna to 17 genera and 51 species. The special
Trilobita, however, number 41 species (6 coming up from the
Tremadoc and 2 passing to the Llandeilo, namely TZrinucleus
Ramsayi and Homalonotus bisulcatus). No group in any of the
British rocks is so specialized as the. Arenig Crustacea. The
Skiddaw rocks hold 9 species, representing 7 genera *; the Shelve
Arenigs have 10 species and 7 generat, both areas showing either
imperfect collecting, or poverty in representation (which is by
no means likely). The few species (mostly single) known or
occurring in each genus clearly shows how large a fauna may
be expected if the more fossiliferous beds could be found in these
somewhat barren rocks. This applies equally to North Wales,
where 9 genera are only represented by 11 ‘species. In South
Wales (St. David’s) the three areas have yielded 15 genera and
39 species. Circumstances have favoured collecting in this re-
gion; and the known fauna is increased thereby. The Northern
or Skiddaw fauna is allied to the Shelve or Shropshire group through
3 species only (Agnostus More, Ogygia Selwynu, and dAiglina
benodosa). The special Skiddaw forms are 4 only (Caryocaris
Wrightu, Phacops Nicholson, Niobe Dovert, and Aglina sp.); but
9 occur in these beds. The special Shelve species are Trinw-
cleus Murchison, Illenus perovalhs, I. Thomsont, and Chewrurus
sp.; but 10 species occur in the Shelve beds. The special North-
Wales species are also only 2, Asaphus affimms and Caryocaris Marrit.
The special South-Wales species are Agnostus hirundo, Asaphus
Homfray2, Ogygra scutatria, O. peltata, O. bullina, Asaphus menapie,
Trinucleus Sedqwickun, Ampyx Salterr, Aiglina bora, 4. grandis, Ah.
obtusicaudata, Barrandia Homfrayr, Calymene ultima, and C. vewata ;
the occurrences in South Wales, however, are 35 species in 15
* Caryocaris Wrightu, Agnostus Moret, Ogygia Selwynit, Trinucleus Gibbsii,
Aiglina caliginosa, Salt., A. binodosa, AL. sp., Phacops Nicholsoni, and Niobe
Doveri.
t Agnostus Moret, Oyygia Selwynti, Trinucleus Murchison, Ziglina binodosa,
Calymene parvifrons and var. Murchisont, Illenus perovalis, I. Thomsoni, Chei-
rurus Frederict, and C. pectinatus.
II4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,
genera. Eleven new genera of Crustacea, 10 of which are Trilobita,
appeared in the Arenig sea: they are Afglina, Angelina, Trinu-
cleus, Barrandia, Calymene, Phacops, Placoparia, Illenus, Ille-
nopsis, Homalonotus, and the Phyllopod Caryocaris, which, with
Placoparia, never passed to higher rocks.
Bracuioropa.—7 genera, Lingulella, Lingula, Orthis, Obolella, Dis-
cina, Stphonotreta, and Dinobolus, represented by only 18 species,
are all that can be recorded of this class through the Arenig rocks.
All the genera and 12 of the 18 species occur in the St.-David’s area.
Only 2 species are known in the Skiddaw rocks, Lingula brevis and
a Discina; and 5 in the beds west of the Stiperstones ; they are
LIingula attenuata, Orthis alata, O. calligramma, O. striatula, and
Obolella plumbea. The 5 North-Wales forms are Lingulellu Davisu,
L. lepis, Orthis lenticularis, O. caligramma, and Obolella plicata,
Tai-hirion yielding 4 of the 5. Lengula petalon, L. brevis, and
Orthis calligramma are all that pass to the Llandeilo rocks; but 9
come from the Tremadoc ; therefore the special forms are only 6—
Siphonotreta micula, Dinobolus Hicksu, Dav., Discina sp., Orthis
striatula, O. remota, and O. alata. The new genera are Dinobolus
and Siphonotreta. ;
LAMELLIBRANCHIATA.—Ribeiria complanata, Modiolopsis trapezi-
formis, Palearca amygdalus, and Redona anglica occur in the
Shelve Arenigs. Palwarca socialis and a species of Ctenodonta occur
only at Ty-obry in North Wales. None are known either in the
Skiddaw rocks or in South Wales, 6 species being the entire bivalve
fauna. ibeiria and Redonia first appear in the Arenig rocks.
GastERoPoDA.—Only 4 genera and 4 species are at present known.
Plewrotomaria Uanvirnensis, Hicks, and Ophileta sp., occur at
Llanvirn, St. David’s ; Rhaphistoma, Skiddaw only; and the Stiper-
stone form is Huomphalus corndensis, Sow. No species known in
North Wales.
Prrropopa,—4 species of Conularia and 4 of Theca constitute
the Arenig Pteropod fauna. ‘The Shelve species are U'heca sumplea,
Salt., and 7. vaginula, Salt. Those occurring in North Wales are
Theca vaginula, Salt., Conularia corvum, Salt., and C. margarite-
fera,Salt. Theca Harknessii, Hicks, T. caereesiensis, Hicks, Conularia
llanvirnensis, Hicks, and C. Homfrayt, Salt., range through the St.-
David’s Arenigs.
Hersropopa.—4 species of Bellerophon in the Stiperstone beds
and 2 in the St.-David’s are all that are known. ‘The Stiperstone
species are B. hippopus, Salt., B. bilobatus, Sow., B. carimarioules,
and B. perturbatus, Sow. The South-Wales species are B. multi-
striatus, Salt., and B. llanvirnensis, Hicks. No species yet known in
North Wales.
CrpHALoropaA.—Orthoceras Avelinit and O. encrinale occur in the
Corndon area (Shropshire). O. sericewm and caereesiense are only
known at St. David’s, South Wales; an undeterminable form occurs
at Ty-obry (Tremadoc, North Wales). None in the Skiddaw beds.
The distinctive value of the Arenig fauna is shown in the fact
that only 8 genera and 9 species pass to the Llandeilo; and 4
ANNIVERSARY ADDRESS OF THE PRESIDENT. II5
of these species are Hydrozoa, 2 are Crustacea (Trinucleus Ram-
sayi and Homalonotus bisulcatus), and 3 Brachiopoda (Lingula
brevis, L. attenuata, and Orthis calligramma). Looking, therefore,
at the number of genera (63) and species (150) in the whole Arenig,
the change or extinction at the close of the period has scarcely
any parallel in the Paleozoic rocks. The accompanying Table
shows the numerical value of the Arenig species, the 63 genera and
150 species being distributed through four well-determined areas,
and showing the fauna to be, in the
Skiddaw beds ...... 31 genera and 49 species.
Stiperstones area .. 26 i Sa ae
North’ Wales’ 202"... 21 A DOr te
South Wales ...... 3o7 i HON a hes
Only 8 genera and 9 species transgressed or passed to the suc-
ceeding formations; and 11 genera and 16 species came in with
the advent of the group from the Lower Cambrian series. The
true numerical faunal value of the Arenig group is therefore 51
genera and 133 species; those forms, or the 9 species, which pass to
higher formations do not affect the Arenig beyond linking it to the
next group in succession.
Taste VIIL—Arenig.
Geographical
Distribution.
: : Pass to
5 . as aR g n |
(o) = [<D)
a5 Ee Sas ie
ro) i) ea 2) :
a 3s . = Wea = iS =a S)
| | eS nD = on (2) oO
Ss SS | eirsh WR Supers ieee i sin |
1/5 ® on ‘2 ‘Ss o 5 a oS
ea Slmia Folalela Oo
Beam ose eet oh Rene a> teers aah alaral Sele
PEO OZOR Aad tassadesoaeat onesies
Ti OZOA Oks v.05. .clotos setae SA Aa sce Mean eae le kee
PACHIMOZOM SG ssc ose sssscheccess soe
Hiehimodermata..........secsss-
9 8 2
PARIMVE NI G reieciS5stsi sic sv eiselddsenieick CS) TE ee es Z
PU RUMCEACEA. 9... ccc acseaeasieesleecec LZ) UG) |) ete ea eee I
BGVOZOA Mec eccctvactnctesddecet.
3 © ee 2 2 3 7 2
ale btaehiOpOda.<........7-.-r0+- +s: Ne Wsh |) A : Bollietael le A
Bamellibranchiata ..........:. A | Or Besee. | lhag 2
| 1 1 2
GaAsKerONOCS .. 05 a.icasde es dear. 4; 4] 3 z meh
2 1 2 2
Peimeecopodari2.. :sstikeeeii:. DAN fo) Z z e
1 i
Te ELC LCLOPOGa4....2:... sesc.08eeees 1| 6 ae ilpcee aleges
MIC CPUMOPOUA 3.:...0c.-25 +e. 52 Missa line 5) 3 zt A
real - A 31 26
Te (PSG 8 ces aed a a G33 ISD) ea ea ee I) a
116 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
LiANDEILO.
It may be thought by some superfluous to discuss the history of
the Llandeilo rocks proper; but it is part of my purpose to do so,
for two reasons :—first, to show their true relations (affinities and
differences) to the Arenigs, which they overlie and with which they
have long been confounded ; and, secondly, to show the geographical
distribution of .the Llandeilo species and their paleontological rela-
tions to the Caradoc rocks above and the Arenigs below. The three
classical localities for the Llandeilo rocks and fossils are Llandeilo,
Builth, and Abereiddy Bay north of St. David’s. Each of these areas
possesses a characteristic and definite fauna ; on the whole the species
in each locality are much the same; still the facies is peculiar in
each. It is also of much interest to clearly understand the true
position of the great band of dark roofing-slate of the ‘ Ffestiniog
quarries” &c. that underlies the Caradoc or Bala series, occupying
the position of the Llandeilo flags. “It is probable that the lowest
portion of the Llandeilo group may occur in the Arenig and Ffesti-
niog mountains, and also in the Arrans ;” but the evidence is slight
and the materials (in the shape of fossils) are scanty. Salter obtained
Bellerophon perturbatus in dark slates near Bangor, and also other
fossils in the slates, identical with those of the Llandeilo rocks,
‘‘ which overlie the Arenig porphyries.” It is doubtful if the
black slates of Anglesey are the equivalents of the dark earthy
slates that range east of the Arenig mountain. The Anglesey slates
contain Asaphus Powis and Phacops apiculatus, both rare in the
Llandeilo group; but the Asaphus occurs both in North and South
Wales, Phacops apiculatus only n Anglesey. The Graptolites, through
Climacograptus celatus(?) and Didymograptus Murchison, distinctly
enable us to refer the beds to the Llandeilo group.
The Llandeilo rocks and their fossils in North Wales are confined to
few localities, and are but feebly exposed anywhere; and the whole
fauna of this formation in that area numbers 47 species. Highteen
of these belong to the prolific class Brachiopoda, 15 to the Crustacea.
The Llandeilo rocks of South Wales contain 88 species; and about
40 are common to North and South Wales. Itis important to show
those species which unite the two areas ; but for my purpose I name
only the Crustacea (Trilobita), Hydrozoa, and Brachiopoda. Of the
former class 8 species are common, viz. Asaphus tyrannus, A.
Powisii, Ogygia Portlocku, Calymene cambrensis, C. Blumenbachii,
Trinucleus concentricus, T. favus, and the Ostracode Beyrichia
complicata. | |
The Hydrozoa are not less important; they are Duplograptus folr-
aceus, D.dentatus, Didymograptus Murchison, Leptograptus flaccidus,
Dicranograptus ramosus, D. formosus, D. Nicholsom, Climacograptus
bicornis, C. celatus, C. confertus, CO. Sharenbergr, and Dicellograptus
sextans.
The Brachiopoda number still more, as we should expect from
their habit and relation to the sea-beds upon which they live. They
are all common and well-known species; and 8 of the 13 forms
ANNIVERSARY ADDRESS OF THE PRESIDENT. Le?
belong to the genus Orthis: they are Crania divaricata, Siphonotreta
nucula, Orthis vespertilio, O. turgida, O. Actonie, O. calligramma,
O. striatula, O. elegantula, O. insularis, O. bifoveata, Strophomena
rhomboidalis, Leptena tenussimistriata, and L. sericea.
Cardiola interrupta is the only Lamellibranch out of the known 6
species, and Bellerophon perturbatus and B. bilobatus the only 2 Hete-
ropoda out of 7, which, with Favosites fibrosus, help to make up the
41 species connecting the North and South Wales Llandeilos; so
that, of the 47 North-Wales species, 40 are common to both areas.
No less than 88 species occur in South Wales. The whole Llan-
deilo fauna for the British Islands numbers 80 genera and 175
species ; of these ] may mention that Ireland has yielded 51 species,
Scotland 66, and Shropshire only 26: these latter are chiefly from
the Shelve district, and are mostly Crustacea and Brachiopoda. Our
knowledge of the number of species occurring in Scotland is due to
the researches of Mr. Lapworth in the Moffat area.
In the St.-David’s area and throughout Pembrokeshire, Brecon-
shire, and Caermarthenshire, the typical localities of Llandeilo and
Builth &c. contain a special fauna. At Abereiddy Bay the black
slates and argillaceous limestones are interstratified with felspathic
tuff; they rest upon the Arenig group, having a distinct fauna; a
thick bed of tuff divides them. The immediate presence and abund-
ance of Didymograptus Murchisom and Dicellograptus, Cryptograptus,
&¢e. in the slates on the south side of Abereiddy Bay above the fel-
spathic tuff, at once clearly marks or determines the base of the
Llandeilo beds.
Dr. Hicks divides the true Llandeilo series of St. David’s into 3
subgroups*, the lowest containing most Rhabdophora or Graptolites,
associated with Trinucleus Ramsayi, Calymene Murchisone, and
Theca caereesiensis, which especially characterize this lower division.
The middle subgroup consists of dark “calcareous shales, with
compact limestone at the upper part;” Asaphus tyrannus, A. pel-
tastes, Calymene cambrensis, Ogygqia convexa, and Trinucleus Lloydu
are the typical Crustacea, with Lingula granulata, Halysites catenu-
latus, and 6 Graptolites. In addition to the fauna, the calcareous
nature of the beds lithologically separates this middle subgroup
from the, over- and underlying series. Everywhere it is charac-
terized by the forms just enumerated ; many of the same occur at
Llandewi Velfrey, Lampeter Velfrey, and Musclewick Bay. The
Upper Llandeilo is also distinguished by special forms of Trilobita
—Barrandia Corda, B. longifrons, Cheirurus Sedqwickit, Ogygia
Buchu, Calymene duplicata, Ampyx nudus, and Agnostus M‘Coyit.
It will be seen that each division is specialized or can be discri-
minated by its Crustacea; the well-known Ogygia Buchu and
Cheirurus Sedgwicki, here as elsewhere, are the typical forms in
the upper black argillaceous slaty flaggy sandstones. The middle
yields Asaphus tyrannus, A. peltastes, and Ogygia convexa, &c. ; and
the Lower Calymene Murchisome and Trinucleus Ramsayi; and
this grouping holds good wherever the Llandeilo beds occur. Three
* Quart. Journ. Geol. Soc. vol. xxxi. pp. 177-180.
VOL. XXXVI.
118 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
species only of Trilobita have occurred in the Scotch Llandeilo rocks,
viz. Lllenus Bowmannu, Salteria involuta, and S. primeva. Ire-
land has 5; but probably many more will occur. I enumerate them
so far as we know them—Acidaspis James, Ampyx mammillatus,
Ogygia Portlocku, Phacops truncato-caudatus, and Avglina mirabilis.
I know no others, although in all the three Llandeilos we have 45
species of Crustacea. Shropshire has only yielded 11 species, and
these chiefly from the Llandeilo rocks of Shelve: they are all marked
species. In the Builth and Llandeilo areas no species occurs below
the tuff-beds of the Lower Llandeilo. Few species of Graptolites
are common to the Llandeilo and Arenig rocks of St. Dayid’s, al-
though here the succession is so complete, and no less than 18
species there occur in the Arenig and 6 in the Llandeilo. Only 16
species of all groups are common to both formations, although the
Arenig fauna numbers 149 and the Llandeilo 175, thus clearly
showing the faunal differences.
Llandeilo beds are known in Merionethshire, Caernarvonshire,
Denbighshire, and Anglesey. Fifteen species have been determined
from Merioneth; 13 from Garn, east of Arenig, by far the largest
fauna in North Wales. Anglesey from five localities yields 15
species and 18 occurrences, or only 3 species for each locality ;
Caernarvonshire, from four localities, 17 species (the chief loca-
lity, Teddyn-Dicum, has produced 8 species); and Craig-y-Glyn,
near Llanrhyader in Denbighshire, 6 species. No one can doubt,
from the above results, that careful research would greatly add to
the faunal value of the Llandeilo rocks of North Wales. Prof.
Hughes has lately succeeded in ascertaining the presence of Tre-
madoc fossils in Anglesey ; and further search at Garn, east of the
Arenigs, could not fail to throw much light upon both the Arenig
and Llandeilo faunas, and to substantiate still more the relation
between North and South Wales. As yet, out of 13 Garn fossils,
we know only 1 Trilobite (Ampya mammillatus). In Anglesey,
near Llanerch-y-medd, out of 5 species collected 3 are characteristic
Trilobites—Phacops apiculatus, Asaphus Powisir, and Calymene cam-
brensis. It is the same with Treiorwerth in Anglesey,—clearly
showing that a rich harvest of Llandeilo species is yet to be ob-
tained in North Wales.
The elaborate researches of Mr. Lapworth, in Scotland*, into the
history of the Rhabdophora of that and other areas, has greatly
modified our views respecting their distribution and range.
The oldest fossiliferous strata known in Scotland are the Grap-
tolite shales forming the well-known Moffat series, a group of black
shales about 600 feet in thickness, and separated by Mr. Lapworth
into three distinct paleontological divisions. The lowest (Lower
Moffat or Glenkiln Shales) he determines to be of Upper-Llandeilo
age; the Middle Moffat or Hartfell Shales above he correlates with
the Bala group of North Wales “as an attenuated representative ;”
and the third or uppermost (the Upper Moffat or Birkhill Shales)
represents the Lower Llandovery. This last determination has an
* Quart. Journ. Geol. Soc. vol. xxxiv. pp. 240-346.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 119g
important bearing upon the distribution of the Graptolithina or
Rhabdophora, it being well known that in the Llandovery rocks of
Wales no Graptolites occur. The Lower Llandovery of Cardigan and
Merioneth, of such great thickness and extent (yet without Grap-
tolites), has ‘‘ dwindled down to the thickness of the Birkhill Shales
(about 70 feet) in the intervening Lake-district, where it constitutes
the Coniston Mudstones—a group of beds almost identical in thick-
ness, lithology, and paleontology with the equivalent Scottish deposit
of the Birkhill Shales” (Lapworth). The conclusion arrived at by
Mr. Lapworth, that the oldest beds of the south of Scotland (the
Glenkiln Shales) are the equivalents of the highest Llandeilo rocks,
is borne out through his researches amongst the Moffat series
in Southern Scotland; and, with him, we must come “to the
conclusion that the Lower Silurian rocks of the southern uplands
can be arranged in two distinct formations, viz. a lower and very
- thin group of fine-grained Graptolite shales, and an upper and com-
paratively massive series of arenaceous strata. In their mineralo-
gical features and paleontological characteristics the Moffat series
differ from any of the typical Silurian rocks of the principality.”
Unlike the rocks of Wales, they are almost exclusively Graptolitie
in their fossil contents, scarcely any Brachiopoda or Crustacea being
known throughout the series. The Llandeilo age of the Lower
Moffat shales is further determined through the total absence of those
complex Arenig forms of “ Dichograpti, Tetragrapti, and Phyllo-
grapti, so characteristic a feature of the Graptolitic fauna of the
Skiddaw, Shelve, St. Dayid’s, and Canadian equivalents.”
Mr. Lapworth, “ arranging the Moffat strata in the order in
which they are displayed, and distinguishing each chief band by its
peculiar fossil,” gives the following Table :—
(Upper Birkhill | Zone of Rastrites peregrinus. \
ir or Grey Shale | Zone of Monograptus spinigerus.
Soa group. Subzone of Diplograptus cometa. | Lower
Birkhill oe 4 \
State Lower Birkhill |) Zone of Monograptus gregarius. Llandovery.
f or BlackShale + Zone of Diplograptus vesiculosus. |
group. Zone of Diplograptus acuminatus. _)
pees eel Zone of Dicellograptus anceps. |
irae Zone of Barren Mudstones. ;
Hartfell 4 stone group. _ { Bal
. Sh, i. \ Lower Hartfell ) Zone of Plewrograptus linearis. r i
a“es- | or Black Shale | Zone of Dicranograptus Clingani. |
{ group. Zone of Climacograptus Wilsoni. }}
Upper Glenkiln
a Fe tiesto | Didymograptus beds. Upper
Tteq, | Lower Glenkiln ) p. Llandeilo.
Shales. SPAlos Ribbed mudstones.
The facies of the Glenkiln shales is distinctively that of the Llan-
deilo of South and North Wales, the assemblage being the same:
differences occur dependent upon locality and the mineral composition
of the beds; but the common Glenkiln forms of Scotland, and those
species collected by observers in North Wales (Messrs. Salter, Hop-
kinson, Homfray, Gibbs, &c.), serve at once to connect and correlate
the faunas of the two areas. 10 species from South Wales and 12
from North Wales are all Glenkiln species and of Llandeilo age;
k 2
I20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
and, adopting the views of Mr. Lapworth, from the absence of
Didymograptus Murchison and the genus Phyllograptus in the black
shales of the Tremadoc area, and the presence of some succeeding
Bala forms, we may infer that these dark Tremadoc shales and the
Glenkiln beds are probably of higher-Llandeilo age. This inference
is further strengthened by researches made by Linnarsson in the
Llandeilo strata “of Central Sweden, where the greater portion of
the Llandeilo formation of Britain is represented by the Orthoceras-
limestone.” ‘‘ Upon this limestone rests the sheet of dark shales
named by Dr. Linnarsson the ‘ Middle Graptolite schists; the
lowest part of these schists, according to Dr. Tornquist, affords
abundant examples of Phyllograptus and the Murchisoni form of
Didymograptus. The highest Swedish beds assigned or referable to
the Llandeilo formation afford both the peculiar Scotch or Glenkiln
and North-Wales forms, such as Didymograptus swperstes, Lapw.,
Cenograptus gracilis, Hall, Climacograptus Scharenbergi, Lapw., C.
perexcavatus, Lapw.
Mr. Lapworth further discusses the relations and affinities of the
Llandeilo species of South Scotland (Glenkiln Shales) with the dark
shales and flagstones of the Cincinnati group which bound the valley
of the Hudson near the. city of Albany and everywhere underlie
the Trenton limestone; he shows reason for believing that we
may regard them as forming the ‘“ highest division of the Quebec
group (Arenig) which emerges unconformably from below the hori-
zontal Trenton limestones. ‘The Hudson-River shales may therefore
represent the higher Llandeilo beds of Britain.” Lapworth names
14 species collected from Norman’s Kiln in the valley of the Hudson,
on the Marsouin river, &c., as being identical with the Glenkiln and
Welsh forms. He still further establishes representative affinity
between the peculiar Glenkiln species which are absent from the
American strata and others which occur in them. Thus :—
BrirTisu. AMERICAN,
Glossograptus Hincksti is represented by Glossograptus ciliatus, Hmm.
Dicranograptus ziczac bs » Dicranograptus furcatus, Hall.
Climacograptus Scharenbergi ,, » Climacograptus scalaris, His.
Clathrograptus cuneiformis ,, » Clathrograptus Geinitzianus, Hall.
‘‘ All evidence, therefore, tends to prove that the Glenkiln shales
belong to the age of the Upper Llandeilo series, and are closely allied
to the North-Wales grouping.” From the absence of certain Dzdy-
mograptt and Phyllograpti from the Glenkiln division, and their
abundance in the lower beds of the Llandeilo of Wales and Sweden,
we are obliged to assign the Scotch Glenkiln Rhabdophora “ to the
highest division of the Llandeilo, and not far below the base of the
Caradoc or Bala’’*.
It is of the Hydrozoa, Crustacea, and Brachiopoda, which together
make up the 123 out of the 175 known species, that the mass of
the fauna of the Llandeilo is composed. The same classes largely
transmit their genera and species to the succeeding Caradoc or Bala
* For an exhaustive paper upon the Graptolites of the Moffat series, by
C. Lapworth, Esq., F.G.S., see Quart. Journ. Geol. Soe. vol. xxxiv. pp. 240-343.
The general characters of the Lower Silurian rocks of Scotland and the strata of ~
the Moffat district are also ably discussed.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 121
rocks, viz. 16 species of Hydrozoa, 17 Crustacea, and 23 Brachio-
peda, or, together, 56 out of the whole 76 that connect the two
formations. It is interesting to know also those areas that are spe-
cifically most prolific in the above groups, and thus help us to draw
conclusions as to the nature of the sea and its bathymetrical condition
during the time of the deposition of the Llandeilo and succeeding
Caradoc, which are more intimately related than is generally believed.
United, the Llandeilo fauna of North and South Wales is constituted
by 94 species; or this is the known number for Wales, 88 occurring
in South and 47 in North Wales, and 41 being common to both,
chiefly among the Hydrozoa and Crustacea. Upon whatever hypothesis
we may account for the physical relationship between the Llandeilo
rocks of Scotland and Ireland, the connecting species are few (only
27); and no Crustacea are common to these two countries—which,
out of a total fauna of 45 species, is remarkable. ‘The Irish species
number 6, 3 of which are also South-Wales forms—Ogygia Port-
locku, Calymene duplicata, and Aiglina mirabilis. As before stated,
Scotland has hitherto yielded only 4 genera and 5 species of Crus-
tacea—lilenus Bowmann, Salteria wmvoluta, S. primeva, Peltocaris
aptychoides, and Discinocaris Browniana.
Praxta.—None.
Proroz0a.—Ischadites antiquus, Salt. No other Protozoon has
been recognized in the Llandeilo; it is not a common genus in the
Lower Silurian rocks.
Hyprozoa.—The Llandeilo beds of Scotland appear to be the most
prolific in Rhabdophora. Our knowledge of them is due to the
researches of Nicholson, Lapworth, and Carruthers in Scotland, all
of whom have done able work in elucidating the history and struc-
ture of this obscure class. Forty-four species illustrate 18 genera ;
but it is chiefly through the larger genera that this Graptolitic fauna
is represented. South Wales, as we should expect, is also represen-
tative, although poor, as compared with Scotland, having only 18
species, or about half the number. North Wales has 7 species, and.
Treland 28. The Welsh and Irish genera have not the same specific
value; generally they are much the same, but illustrated by fewer
species. This may be due to want of systematic search in Wales,
such as the rocks of Scotland have undergone by the above-men-
tioned authors. The genera Didymograptus, Diplograptus, Climaco-
graptus, and Dicellograptus are those chiefly occurring in South
Wales; and Diplograptus, Dicellograptus, and Climacograptus in
North Wales, &c. The Llandeilo rocks of Ireland contain species
of nearly all the above genera. ‘Thus of the 44 known Llandeilo
Rhabdophora we have
Species.
Ouse WMeS ee. 6.4. Sooke craye Bue 18
INO rb NWiale sues cc Bac a ee o
SCO bam sees tie eR Bu
Nereida See wi,.. & wa vets 28
85 occurrences ;
and 16 species pass to the succeeding Caradoc.
122 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Actrnoz0a.—Halysites catenulatus, Linn., Favosites fibrosus, Goldf.,
and Monticulipora favulosa, Phill., complete the list of the Llandeilo
Actinozoa. No English form is known. North Wales yields Favo-
sites fibrosus. All three occur in South Wales, and Fuvosites fibrosus
in Ireland. Scotland has no representative. All three species pass
to the Caradoc. These are the first corals occurring in the British
rocks ; but they expand to 20 genera and 42 species in the succeeding
Caradoc. We cannot admit that change of condition only thus
favoured the growth and development of the Actinozoa. It is true
little limestone occurs in the Llandeilo, and that little in the upper
division; but the organic remains in the Upper Llandeilo limestones
are chiefly Crustacea. The increase of limestones and calcareous
matter in the Caradoc rocks being due to life agency, we may
attribute much of it to the secretion of carbonate of lime by the
Coelenterata. The only notable or appreciable form is Halysites,
which was abundant.
Ecutnopermata.—We know of only 4 genera and 4 species of
this class, which, like the Actinozoa, may be said to first appear in
the Llandeilo. None are known in the Arenig below; but 4 species
(1 Menevian and 3 Tremadoc) in fragments have been preserved in
older formations. The 4 Llandeilo species are Actinocrinus Wynne,
ichinospherites granulatus, Paleasterina Kinahan, and Glypto-
crinus basalis. The first 3 are Irish; Glyptocrinus occurs in the
South-Wales Llandeilos. Two of them passed to the Caradoc. As
with the Actinozoa, this group became greatly developed in the
Caradoc, no less than 15 genera and 32 species enriching that for-
mation. ‘These, like the corals, must have lived in a moderately
deep sea well charged with calcareous matter.
ANNELIDA.—It is questionable if more than 6 species (although
9 are placed in the Llandeilo) occur: Paleochorda teres, P. major,
and P. minor may be Arenig; they are very sparingly distributed,
only 1 species occurring in England, South Wales, and North Wales,
and 2 in Scotland. I know of no Irish Llandeilo Annelida.
Crustacea.—In this class the Trilobita are of high significance,
in both the Llandeilo and Caradoc formations, especially the latter,
in which we know of more than 100 British species. The Llandeilo
rocks have yielded 18 or 20 genera and only 45 species, or upon
the © igs only about 2 species to each genus. Many genera are
represented only by 1 species; these are Homalonotus (H. bisul-
catus, Salt.), Lichas (L. patriarchus, W.-Kdg.), Stygina (S. Murchi-
sonic, Murch.), Oheirurus (C. Sedgwickit, M‘Coy), and Acidaspis (A.
Jamesti, Salt.). Much has yet to be done by collectors to increase
our knowledge of the specific crustacean fauna of the Llandeilo rocks.
South Wales being the classical locality for the Llandeilo group, it is
natural that we should expect to find there the largest and most
typical fauna, crustacean or otherwise. In one group (Graptolites)
we have seen that this is not the case, Scotland being most repre-
sentative. Here, however, the Crustacea of South Wales (29
species) are double those of North Wales (15), and ten times more
than those of Scotland, which has yielded only 3 species, conditions
ANNIVERSARY ADDRESS OF THE PRESIDENT, 123
being more favourable for the support and distribution of certain
forms of life in one area than the other. The only 3 Scotch Llan-
deilo species known to me are Jilwnus Bowmanii, Salt., Salteria
wnvoluta, Thom., and S. primeva, Thom. The 6 Irish species
are Acidaspis Jamesii, Ampyx mammillatus, Ogygia Portlocki,
Phacops truncato-caudatus, Calymene duplicata, and Aiglina mirabilis.
The English forms are chiefly from the Shelve area; and 8 out of
the 10 are South- Wales species.
The following occupy and characterize definite areas; they are
single representatives of the genera named :—
ae aoe England.| Scotland.) Ireland.
Homalonotus bisulcatus...... *
menostus Mi Coyi) s....-1.-..- Pe *
Stygina Murchisone ......... : *
Cheirurus Sedgwickii......... soo *
Acidaspis Jamesii ............ Sas a wh Acts %
Lichas patriarchus ............ "stg *
1 4 il
Thus 6 Llandeilo genera are illustrated by only 1 species each,
England and Scotland having no really marked or characteristic
form. Nevertheless there are important Llandeilo species which
are entirely restricted to that formation, not ranging either lower
or higher. The most important are :—
North | South |
Wales. Wales, Hie Tana (Secktind | Ireland.
Illznus Murchisoni .........
Ogygia angustissima .........
—— Portlockii ...............
——= COINCeENSIS .........0.000.
AD WCHM ays slag ost eee aides
COMVOMAN io. oe cc cece:
Asaphus tyrannus ............
EMGASTES) seo askc.dsectewe-
datveostatus.....-.sc-.9a<s: ;
Calymene cambrensis ...... *
Trmucleus Lioydu............
IUAMING AWG eicline seen delice
MUSEUM ES . castscce. ves
VENTE! Gate GOns ee ermprerere
KK OK
kK KK Ss
* OK KOR:
5 re
KK OK OK kK KS ft
KOK
Ks °
*
Kk
%
AGIIAMGP sere aeecd sew elelse we 3
*
I24 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
All the above 20 species are confined to the Llandeilo and to the
geographical areas assigned to them, and they are essentially cha-
racteristic ; the remaining 15 species pass to the Caradoc, and are
therefore of no value stratigraphically. To complete the analysis
of the distribution and value of the Crustacea I name the 15 species
that connect the Llandeilo and Bala formations :—
Acidaspis Jamesii. Calymene Blumenbachii.
Homalonotus bisulcatus. brevicapitata.
IWenus Bowmanni. Trinucleus fimbriatus.
Ampyx mammillatus. —— concentricus.
rostratus. Phacops apiculatus.
nudus. truncato-caudatus.
Asaphus Powisii. /églina mirabilis.
Calymene duplicata.
The singular Phyllopod Peltocaris aptychoides occurs both in Scot-
land and North Wales, and is not known out of the Llandeilo beds.
Bracutopopa.—This class is an important factor in the Llandeilo
rocks; 10 genera and 34 species are known. Five new genera appear,
Acrotreta, Orania, Rhynchonella, Strophomena, and Leptena; the
first 4 with a single known species only; but Leptena has yielded
4 species, all of which occur in South Wales, and 2 of them in North
Wales. As we should anticipate, the species are most numerous in
South and North Wales. The former area gives us 26 species, the
latter 18 ; Scotland 9, and England 6. Although there are 20 species
in the Arenig group (and 34 in the Llandeilo) yet no species 1s common
to the two formations, no Arenig form passes up; but of the 34
Llandeilo forms, 23 pass to the Caradoc. ‘This is chiefly through
the genera Lingula, Orthis, and Leptena—A4 out of 6 in the former
genus, 11 out of 13 in Orthis, and all the known 4 in Leptena.
We have already seen that of the whole fauna of the Arenig (150
species) only 17 pass up into the Llandeilo; whereas no less than 72
out of 175 Llandeilo species are found in the Caradoc, viz. Hydrozoa
16 species, Crustacea 17, Brachiopoda 23, Bivalvia 3, Gasteropoda 4,
Heteropoda 5, and Cephalopoda 2. The remaining forms are dis-
tributed through smaller classes. But for the distinctive character
of the Abereiddy-Bay and Caermarthenshire faunas, there is much
that is common between the Llandeilo and Caradoc.
LAMELLIBRANCHIATA.—With the exception of the Irish species
Pleurorhynchus calcis, Baily, allthe Bivalye Mollusca known are from
the South-Wales Llandeilos. We know of no Llandeilo Pelecypod
mollusk either in England or Scotland. Cardiola interrupta occurs
in both North and South Wales; Modiolopsis expansa, M. inflata,
Ctenodonta varicosa, and Palearca amygdalus only in the South-
Welsh beds. Three pass to the Caradoc. Pleurorhynchus and Car-
diola are new genera.
GastERopopa.—South Wales has hitherto only given us 1 species,
Murchisonia simplex, M‘Coy; Ireland 2, Huomphalus parvus, Portl.,
and Twi'bo tritorguatus, M‘Coy; the Shelve area and North Wales
Cyclonevva crebristria, M‘Coy, and Ewomphalus corndensis, Sow., the
ANNIVERSARY ADDRESS OF THE PRESIDENT. 125
remaining 7 being from the Durness limestone of Scotland (they may
be Arenig). The Scotch species are Huomphalus matutinus, Hall,
Murchisoma angulocincta, Salt., MW. angustata, Hall, WM. bellicincta,
Salt., MZ. gracilis, Hall, Ophileta compacta, Salt., and Pleurotomaria
thuli, Salt. Three of the 12 pass to the Carodoc. Huomphalus,
Cyclonema, and Murchisonia are new genera, and first appear in
the Llandeilo.
Prrropona.—Three species of T’heca—T. cometoides, Baily (Irish),
T. reversa, Salt., and 7’. caereesiensis, Hicks (from St. David’s). No
species occurs in England, North Wales, or Scotland.
Hurrrorops.—sScotland possesses 5 of the 7 species known ; and
4 of the 5 are Macluree. These are associated with the Gastero-
poda in the Durness limestone. Bellerophon perturbatus is a North
and South Welsh species ; and B. bilobatus, English, North and South
Welsh also. Huomphalus scoticus is from the Ayrshire rocks, The
3 last-named species and Heculiomphalus pass to the Caradoc.
CrpHALopopa.—Of the 3 genera and 7 species none occurs either
in North Wales or Ireland. The only English species is Orthoceras
Avelani?, Salt., from the Shelve area (Shropshire) ; Endoceras eoum,
Edgell, is from South Wales. The remaining 5 of the 7 known
species are Scotch, including the singular genus Piloceras (P. in-
vaginatum) from the Durness limestone.
The accompanying Table (p. 126) gives the following results.
The 12 zoological groups occurring in the Llandeilo rocks are re-
presented by 80 genera and 175 species, which are numerically
distributed as follows :—
England .... 18 genera and 26 species.
North Wales; 30. ieee 3
South Wales.. 47 ,, RS OR: =.
Scaulandiy hey sok
itrelandiy ss 24: SOs SAU Pg
38 genera and 73 species of the 175 pass to the Caradoc. It
will be seen that it is through the Hydrozoa, Crustacea, and Bra-
chiopoda that the community of species largely occurs between the
Llandeilo and Caradoc generically and specifically—through the
Hydrozoa 9 genera and 16 species, the Crustacea 9 genera and
17 species, and the Brachiopoda 7 genera and 23 species. ‘The re-
maining passage numbers are seen in Table IX.
From Arenig.
AL
© bo
© 0
126 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Taste [X.—Llandeilo.
Geographical Distribution.
n a 3
oS oi ro a a a) cs =
: 2 = > | & = a se
Classes. © 5 = a = Ss ae
; 2 ep = o Ay &
5) 2, = =| pics| ° LY ‘S)
O wD = 3 = =
cS B Es R = °
i) -
Zz mM
Plante.
(PEOLOZOd: Wiaewae eee 1 1 a
eerseeceeoree 4 5 1 4 1 3 Z 4 2
Hydrozoa 18 44 a : 18 aS 28 16
. 1 3 3
ACHINOZOR 2. e2s se 3 3 ae : 3 A 3
Echinodermata...... i 4 1 is } cae d 2
j 1 1 i 2
AMMeli Gay seacoast 6 9 2 i 1 3
sta 6 ie) 12 4 9
Crustacea ele Seiwidiolalai ovate 20 45 10 ; 5 29 5 é ry
Bryozoa.
ng ahi 2 6 8 4 4 Cf
Brachiopoda ......... 10 34 r 18 25 9 9 23
Lamellibranchiata. . 5 6 fh A 4 1 3
2 1 2 2
Gasteropoda ......... 6 12 2 1 i 7 2 3
1 1 1
Pteropoda ....d24.065% 1 3 de B. A ies 7 :
1 1 1 2 2
Heteropoda ......... 3 a ; 2 2 3 i 4
Cephalopoda......... 7 ; 1 é 1
Wh 18 27 47 31 31 38
aogooosas 80 1 (Oo 26 47 87 66 51 73
Carapoc or BAta.
The rocks overlying the Arenig and Llandeilo groups, and under-
lying the May-Hill Sandstone, have received much critical attention
from Sedgwick, Murchison, M‘Coy, Salter, and the officers of the
Geological Survey. The facies of the fauna is that of the Llandeilo,
but greatly developed. The increased fauna of the Caradoc is
scarcely recognized until subjected to critical research and analysis.
The difference in the fossil contents of the two groups is due chiefly
to age and the conditions under which they were deposited. Sedg-
wick, in 1853, placed the Bala group in his ‘‘ Upper Cambrian ”
division, dividing it into Lower, Middle, and Upper Bala; it in-
cludes also the ‘Cambro- Silurian of some authors, a term used or
adopted by Prof. Jukes in his ‘ Manual of Geology.’
From the year 1832 to 1853 Sedgwick included the Caradoe in
the term “ Lower Bala,” not ieee then the existence of the
term Caradoc. Sir H. de la Beche, Prof. J. Phillips, and the Survey,
from 1840 to the present date, designate this formation the ‘Caradoc
or Bala.” Murchison, from 1831 to 1859, used the term “‘ Caradoc
ANNIVERSARY ADDRESS OF THE PRESIDENT. 127
Sandstone.” The term Llandeilo was not admitted by Sedgwick
either in the ‘ Synopsis’ or the Woodwardian Catalogue ; therefore
great difficulty was and is still felt as to the identification of species
long ago collected in certain localities, especially those having
reference to the Lower “ Llandeilo of Murchison ” and the Arenig
of Sedgwick; the faunas of all three groups require careful revision,
in consequence of old or early errors, which of necessity demand it.
Sir Roderick Murchison, in 1833, first noticed the ‘ Caradoc
Sandstone ”’*; in 1834 the same rocks were described by him under
the name of the “ Horderley and May-Hill Sandstone.” In the
‘Silurian System,’ subsequently published, these strata were called
‘Caradoc Sandstone,” the name being based upon their being highly
developed in the neighbourhood of Caer Caradoc.
In the early history of the Caradoc rocks the fossils of the
Pentamerus-beds were included in its lists. The Survey subsequently
corrected this, by separating the upper part or highest beds of the
Caradoc. In 1852 Prof. Sedgwick and Mr. Salter in part corrected
this error, and showed that the fossils of the May-Hill group were
very distinct from those of the Caradoc Sandstone. Again, the
upper Pentamerus-beds rest unconformably on the true Caradoc
Sandstone, and the whole pass under the Wenlock Shale. In
Shropshire and at Builth the unconformity is visible; and in the
Malvern area, west of the Herefordshire and Worcestershire Beacons,
the Upper Llandovery beds lie directly upon the Upper Lingula-flags
or “‘ Dictyonema-shales.” Again, the Upper Llandovery beds on the
banks of the Onny river lie on the upper part of the Caradoc
or Bala beds. West of Wenlock Edge they cover the nearly vertical
edge of the Cambrian or Longmynd rocks. “ Probably,” says Prof.
Ramsay, “there is no unconformity so complete yet observed in
other members of the British Silurian strata.” Besides the researches
and large collections of fossils made by the Survey from these
rocks, the labours of Sedgwick are preeminently associated with the
Caradoc and Bala beds of Wales, through the great memoir on the
British Paleozoic Fossils, in which he was so well aided by Prof.
M‘Coy, and the “ Woodwardian Catalogue” ft prepared by Salter
from the great store of materials in the Woodwardian Museum at
Cambridge, and which, many years previously, he had helped
Sedgwick to collect, and name, from the classical localities in Wales.
To Prof. Ramsay, for his valuable memoir on the Geology of
North Wales+, every student is deeply indebted. In this great
treatise every detail relative to the physical history and distribu-
tion of the Caradoc and Bala rocks and fossils is treated upon ;
and to the appendix, originally compiled by Mr. Salter, I have
greatly added, especially in that portion treating of the distribution
of life, not only for the Caradoc, but through the whole of the for-
* Proceedings of the Geological Society, 1833, vol. 1. p. 476.
t ‘A Catalogue of the Collection of Cambrian and Silurian Fossils contained
in the Geological Museum of the University of Cambridge.’ By J. W. Salter,
F.G.S. With a Preface by the Rev. A. Sedgwick, LL.D., F.R.S.
¢{ Mem. Geol. Surv. of Great Britain, vol. iii. Geology of North Wales.
128 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
mations of North and South Wales. The portion of the memoir by
Prof. Ramsay devoted to the Caradoc is of necessity large, arising
from the extent, magnitude, and importance of the Caradoc rocks
as developed in North and South Wales, Westmoreland, Ireland,
and Scotland. I therefore, as in the case of the older groups, com-
pare or attempt to correlate other portions of Britain with the
typical area in Wales, so as to show the present aspect or distribu-
tion of the Caradoc fauna, which is so largely developed in the
British Islands. To devote much space to the purely geological
aspect of the Caradoc would be needless under present circum-
stances, as so much has already been done by able observers in the
pages of our Journal, as well as in the exhaustive memoir on North
Wales by Prof. Ramsay. My tabular results in the appendix to the
above memoir, relative to the distribution of the Caradoc fossils both
in time and space, will, when published, embody almost all the in-
formation known. ‘The result, however, will be referred to here, as
being a complete analysis of the 600 species. It is scarcely neces-
sary for me to discuss the views of authors as to very minute sub-
divisions of the Caradoc group in any given area or under any
peculiar condition ; such will always arise under critical examina-
tion, extended knowledge, or constant research ; and large as we know
the fauna to be, owing to the rocks being so extensively worked in
the days of Sedgwick and Murchison, and through the long-con-
tinued labours of the Geological Survey, yet many of the zoological
groups are still being added to. This is notably the case with the
elaborate memoir upon the Girvan fossils by Prof. A. Nicholson and
Mr. Etheridge, jun., the first volume of which, containing this
addition to our knowledge of the Caradoc fauna of Scotland, is just
completed and published. In this work the authors describe 41
genera and 65 species, many of which are new. Perhaps, with the
exception of Mr. Lapworth’s paper on the Graptolites of the Moffat
series at Girvan and Glenkiln* (mostly Lower-Bala or Llandeilo
_ forms) no more important addition to our knowledge of the Caradoc
fauna has been made since M‘Coy completed his great work upon
the British Paleozoic fossils.
The legends attached to the published maps of the Geological Survey,
and the explanation of the colours employed to designate the horizons
or formations surveyed, show that no attempt was made by the Survey
to divide the Caradoc rocks into subgroups, or into Lower, Middle, and
Upper Caradoc or Bala; neither does Prof. Ramsay, in that part of
his memoir devoted to the Caradoc rocks, attempt any subdivision,
but masses the whole group between the top of the Llandeilo and
the overlying Llandovery. In the Catalogue of the Cambrian and
Silurian fossils in the Woodwardian Museum, Cambridge, Prof.
Sedgwick has divided the Bala beds into three subgroups, placing
them in his Upper Cambrian stage (the Cambro-Silurian of some
authors), the Lower Silurian of Murchison. The grouping adopted
in this catalogue is such as to eliminate the true Llandeilo fossils,
* Quart. Journ. Geol. Soc. vol. xxxiy. pp. 249-346.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 129
and place them in his Lower Bala group. The Bala group, or
Upper Cambrian of Sedgwick, consists therefore of
( Lower Bala= Llandeilo flags (Upper Llandeilo of the
| Geological Survey, the Arenig being the Lower).
Upper | Middle Bala=the Caradoc Sandstone and Bala rocks
Cambrian *. § (Geological Survey and Sir R. Murchison).
| Upper Bala=the Caradoc Shales, Hirnant Limestone,
| and Lower Llandovery rock (Geological Survey).
The Upper Llandovery or May-Hill Sandstone unconformably over-
lies these.
Sedgwick’s Middle Bala, and part of the Upper, are therefore
equivalent to the true Caradoc of the Geological Survey; and as
such I treat that group here; or the Middle Bala of the Cambridge
Catalogue will embrace the whole of the 600 species known as
Caradoc forms. I have already discussed the Llandeilo formation
proper in the sense now used by the Geological Survey, having
relegated those species hitherto called Lower Llandeilo to the Arenig
group—the Middle Cambrian of Sedgwicky. The Lower Bala
includes certain dark earthy slates and bands of limestone occurring
on the east flank of the Arenigs, Mynydd Tarw and Craig-y-glyn
above Llanarmon in the Berwyns, the black slates on the flanks of
Snowdon, also the arenaceons deposits on the west side of Bala Lake
below the Bala Limestone, and that limestone also.
The Middle Bala group of the Woodwardian Catalogue embraces
the Bala Limestone and its associated sandstones and slates in North
and South Wales. In Shropshire it is the Caradoc Sandstone, with
its Horderley Limestone. The Coniston and Kildare limestones, and
the Craig-Head and Peebles limestones, are all of this aget.
Sedegwick’s ‘“‘ Upper Bala” comprehends the Aber-Hirnant beds
above the Bala Limestone (with peculiar fossils), the lower part of
the Coniston Flags (that conformable to the hmestone), and all beds
above the Bala Limestone and beneath the May-Hill Sandstone.
Again, the ‘‘ Upper Bala” includes all the beds, whether near
Meifod or Welchpool or Llanwyddyn, which lie above the Bala
Limestone and under the unconformable cover of the Denbighshire
grit and flag. In ascending order the Upper Bala includes
(1. The Hirnant Limestone and slate=Coniston Flags,
| lower part only (Ashgill, Coldwell, &c.), above
the Coniston Limestone.
(Sedgwick). | 2. Llandovery beds (Lower Llandovery of Murchison)
2 eh =the Mathyrafal Limestone, near Meifod, of
\ Sedgwick.
“Tt is the great fossiliferous group of Haverfordwest. The
Daiquorhan and Mullock beds in Ayrshire, the fossiliferous rocks of
Maume and Cong in Galway belong in part to it’’§.
* Vide Woodwardian Catalogue, Cambridge, pp. 25, 26, &e.
T Consult the table of equivalents of the strata underlying the May-Hill
Sandstone, Woodwardian Catalogue, p. 25.
t Vide Woodwardian Catalogue, pp. 26, 39. § Loe. cit. pp. 26, 72.
130 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,
It has been stated that the fauna of the Llandeilo rocks num-
bers 80 genera and 175 known species. The Caradoc or Bala
contains 179 genera and 613 species; or 88 new genera and 375
new species make their appearance either at the close of the
Llandeilo or during that period which ushered in or brought about
those changes of conditions under which the deposits of the Cara-
doc sea were accumulated and its species developed and multiplied,
covering as it does so extensive an area in Kurope and Britain, also
extending to America, whether homotaxially in that region or con-
temporaneously with the deposition in the British area it is difficult
to say. That the Trenton and Hudson-River group of North
America, and nearly the whole of the Ktage D of Barrande (Bohemia)
and Regio D of Angelin (Sweden), are the equivalents of our great
Middle Caradoc and Bala, or the true Caradoc, is now not doubted.
The fauna of the Bala group, especially in its zoological groupings,
differs much from the preceding Llandeilo, although many species
(85) are common to the two formations.
I purpose treating of the Caradoc rocks and their fossils at some
leneth—their stratigraphical place, the geographical distribution of
their fossils (especially with reference to the succeeding Lower and
Upper Llandovery)—questions which demand critical examination
or analysis.
The three classes having the greatest number in common are the
Hydrozoa (Rhabdophora), the Crustacea (Trilobita), and the Bra-
chiopoda. The number of known species in the Llandeilo in each
of the above classes is
Ey droZz 0a; tert ven.rteee ee 44
Crugtaces ene ee 45
Brachiopeda 1.232% .): 34
In the Caradoc fauna the same three classes number, including
those from the Llandeilo,
Hydrozoay 2a 38
Crustacea y cee mnne 146
Brachionodan @siosaec. 109
Numerically, the remaining ten classes have little value for compa-
rison, although the Actinozoa, Echinodermata, Lamellibranchiata,
and Gasteropoda are well illustrated (see Table X.). It is through
the above three extensively developed groups, which are mainly
moderately deep-sea forms, that the two formations are united.
The fact of 73 species out of 175 passing from the Llandeilo to
the Caradoc is highly suggestive, and is confirmatory of the views of
Sedgwick in uniting the Llandeilo to the Lower Bala; and the
distinctiveness of the great Middle Bala is confirmed by the fact
that, out of 610 species in that formation, only 102 pass to the Lower
Llandovery. Therefore, on paleontological data, we may regard the
Llandeilo and Caradoc as being most closely allied. The 102 trans-
gressive Caradoc species are distributed through the following
classes :—
ANNIVERSARY ADDRESS OF THE PRESIDENT. 131
12h: Y.-C) 1 out of 10 known. )
FIVOEOZOG. 2. i nus ly PETG)
Colenterata ...... Die eri GOs, |
TES Cree Often tN:
iRehinedcrmata ucts 721) 496 (O20 ols,
Weushacka, uiis.6 NG. De eA Pass to TL,
12 \1(07 20 er eee ee Al Dial 3 = ‘ d ie
Pe brachiOpodan sca 93°. 55) LOD) «3, BNET
Hamellipranchiata... 3 -,,« 76 «,,
Gasteropoda ...... LO eS 08,5
Pieropoda: 4.5.0. - thin ates hy D7 net 9 25
Heteropoda ...... Lp pestn whois
Cephalopoda ...... Tie nA] lt.
ee
OGIO’ wiz:
The important zoological groups in the Caradoc are therefore the
Hydrozoa, Coelenterata, and Echinodermata—the latter especially
through the Cystideans, no less than 8 genera and 23 species illus-
trating thisrare group. The Crustacea number 146 species, of which
106 are peculiar; 20 species are from the Llandeilo and 16 pass
upwards to the Lower Llandovery, leaving thus for the Caradoc
and Bala beds the largest Crustacean fauna known in the Lower
Palzozoic rocks. Only 4 species of Bryozoa out of the 21 appear to
pass to the Lower Llandovery; and they all commence in the
Caradoc: they are Fenestella subantiqua, d’Orb., Ptilodictya dicho-
toma, Portl., P. coslellata, M‘Coy, and P. lanceolata, Goldf. We
should expect more species in common in this group, from the fact
of their being usually a moderately deep-sea family, and less subject
to vicissitude or change than littoral or sublittoral species. The -
Brachiopoda of the Caradoc and Bala group number 109 species,
representing 16 genera; they are more numerous than in other of
the Paleozoic rocks. 33 of the 109 pass to the Lower Llandovery ;
and we have seen that the connexion with the Llandeilo below is
through 26 species, leaving, therefore, 50 as Caradoc proper. As
regards geographical distribution, North-Welsh forms greatly pre-
dominate, owing probably to the larger amount of research to which
the rocks of the four counties of Caernaryon, Denbighshire, Mont-
gomeryshire, and Merioneth have been subjected. Ireland also has
yielded 60 species, and Scotland 40. Their more gomrighee distribu-
tion will be further discussed under that head.
The littoral or shallow-sea condition of the Caradoc is further
illustrated by the occurrence of a large number of bivalve Mollusca.
No less than 76 species are known; and of these only 3 species pass
to the Lower Llandovery, viz. Pterinea retroflewa, Wahl., Orthonota
suleata, His., and Mytilus mytilimeris, Cony. ; and 2 of these 3 forms
pass to the Ludlow and the Upper Llandovery, viz. Pterinca retroflexa
and Mytilus mytilimeris ; so that 66 species of Lamellibranchata be-
long to the Caradoc exclusively ; and, strange as it may appear, these
3 are the only species known im the whole of the Lower Llandovery.
132 PROCEEDING OF THE GEOLOGICAL SOCIETY.
The Bivalvia of the Caradoc exceed in number those of any other
known formation below the Carboniferous Limestone. Careful analysis
shows that the Arenig rocks contain only 6 species, the Llandeilo 6,
the Caradoc 76, Lower Llandovery 3, Upper Llandovery 29, Wen-
lock 45, and the Ludlow 71 species; about 13 species range from
the Caradoc upwards or through to the Ludlow, 7 to the Upper
Llandovery, 3 to the Woolhope, 11 to the Wenlock, and 12 to the
Ludlow—this of course being inclusive, as some of the same forms
appear more than once in their range. It is not improbable that
errors as to species occur, especially when we have to do in many
instances with mere casts in these arenaceous deposits. In both the
Lower and Upper Llandovery groups the fossils are badly preserved,
being casts only. If the Lamellibranchs are largely represented in
the Bala group, the Gasteropoda are almost equally so, by 14 genera
and 53 species; 2 only (Murchisona simplex, M‘Coy, and Turbo
tritorquatus, M‘Coy) are common to the Llandeilo below; 10 pass to
the Lower Llandovery ; 9 direct to the Upper Llandovery ; 7 species
are common to the Caradoc, Lower Llandovery, and Upper Llan-
dovery ; they are Cyclonema crebristria, M‘Coy, Holopella cancellata,
Sow., H. tenuicincta, M‘Coy, Murchisonia cancellata, M‘Coy, MM.
pulchra, M‘Coy, Trochonema triporcatum, M‘Coy, and Rhaphistoma
lenticulare, Sow. Only 3 species pass to the Wenlock rocks: one
of these is Holopella cancellata, Sow. ‘The Gasteropod fauna there-
fore is as significant as the Lamellibranchs, no fewer than 32 of
the 53 species being confined to the Caradoc or Bala group. 16 of
the 53 are peculiarly Irish forms, and 5 Scotch, leaving 21 for dis-
tribution through the North- and South-Welsh and English beds, of
which 9 occur in the Caradoc of Shropshire. I have no determined
species from Westmoreland ; North Wales yields 26 species, South
Wales only 3, viz. Cyclonema crebristria, Holopella cancellata, and
Patella saturni, and these only in Caermarthenshire. This group,
like the bivalves, indicates shallow-water conditions.
The Pteropoda (4 genera and 12 species) are, with 4 exceptions,
confined to the Caradoc. Conularia Sowerbyt passes to the Lower
Llandovery, Wenlock, and Ludlow ; ELeculeomphalus scoticus, M‘Coy,
is Llandeilo and Upper Llandovery ; 9 of the known species are
Irish, and 3 of them Scotch; so that the Lower Llandovery is only
directly allied to the Caradoc by one form (C. Sowerby) out of
the 12 occurring. This is even more strongly manifested by the
associated’ class Heteropoda, of which, as in the Pteropoda, only 1
species in 15 passes to the Lower Llandovery—Bellerophon carinatus,
Sow., being, so far as I know, the only form in this group connecting
the two formations. Bellerophon bilobatus, Sow., B. perturbatus, Sow.,
and Maclurea macromphala, M‘Coy, are also Llandeilo. The Upper
Llandovery has 3 in common, Woolhope 4, Wenlock 2; and 2
pass to the Ludlow. Specifically, 6 pass up, leaving 8 as be-
longing to the horizon. The Pteropoda, being strictly or essen-
tially pelagic, give us little clue as to bathymetric conditions at
the time of deposition. Neither do the Cephalopoda; but no single
class is so preeminently Caradoc: of the 47 known species, only 1
ANNIVERSARY ADDRESS OF THE PRESIDENT. 133
(Orthoceras arcuoliratum, Hall) unites it with the Llandeilo group
(and this I believe to be a doubtful species); and only 7 connect it with
the Lower Llandovery, and 3 of the 7 do not range higher. The 7
species are Jituites cornu arietis, Sow., Orthoceras ibex, Sow., O.
vagans, Salt., O. annulatum, Sow., O. Barrandu, Salt., O. politum,
M‘Coy, and O. tenuistriatum, Minst. The 3 species that directly
unite the Caradoc and Lower Llandovery are three of the above—
O. vagans, Salt., O. annulatum, Sow., and O. Barrandii, Salt. 9
range to the Upper Llandovery, 4 to the Woolhope, 9 to the Wenlock,
and 3 to the Ludlow. These are the appearances of species that
ascend through and into the higher formations. 30 of the 47 species
are confined to the Caradoc, not ranging higher, whereas 15 species
pass to the rocks above. Ireland is represented by 24 of the 47
species, 18 of which do not leave the Caradoc horizon, and 17 are
strictly confined to the Irish deposits.
Of the Scotch Caradoc Cephalopoda we only know of 6 restricted
species, viz. Orthoceras audax, Salt., O. arcuoliratum, Hall (also
Llandeilo), O. vaginatum, Schloth., O. politum, M‘Coy, O. prumevum,
Forbes, and O. tenwistriatum, Munst.; and only 15 species out of the
known 47 occur in the Scotch rocks.
GEOGRAPHICAL DISTRIBUTION.
I have now to treat of the geographical distribution of the
extensive series of species occurring in the Caradoc and Bala rocks,
the large fauna (614 species) being an additional reason for so doing,
more especially considering the widely spread area occupied by the
Lower and Middle Bala groups. It would be impossible to give ali
the localities whence our knowledge of their distribution has been
_derived; but the chief in North Wales number between 30 and 40,
and in South Wales about 10. The Shropshire and Westmoreland
localities are less numerous, but are prolific in species.
The following 10 areas, including about 50 localities in the British
Islands, have yielded the 613 species known. Their occurrences or
appearances number 1555.
- ( Caernarvonshire......... 105 species, distributed in 10 chief localities.
North } Denbighshire ............ 131 af ° Ghees -
Wales. | Montgomeryshire ...... 1388 4 Be is A 3
Merionethshire ......... 162 Fe i LOweaes $3
South { Pembrokeshire ......... 93 es Ms Rn iss Pe
Wales. Neer ccchirs mere 72 fs a pes 6
end leeresie ara Poe aces os: 123
8 * | Westmoreland ...... 123
SUC ENING | Goh SAS COREG REEMA aEEe Bere 302
[iyailninG! CL EAe seer 306
1555
The actual number of species (so far as we know) occurring in
North Wales is 270, in South Wales 134, in Shropshire 123, in
Westmoreland 123, in Scotland 302, and in Ireland 306.
The intimate relation of the Caradoc to the succeeding Lower
VOL. XXXVII.
134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Llandovery rocks obliges me to show their specific affinity, for the
purpose of ascertaining the paleontological value of the Lower Llan-
dovery (the Upper Bala of Sedgwick). Analysis shows that, of the
613 Caradoc species, 103 pass to the Lower Llandovery ; but, strange
as it may appear, 107 are common to the Caradoc and Upper Llan-
dovery, although we know of the stratigraphical break that occurs
between the two formations. This relation is chiefly through the
Actinozoa, Hydrozoa, and Brachiopoda, as we might expect from their
bathymetrical position and habitat.
Of the 40 known corals, 22 (or more than one half) range to the
Llandovery rocks, 20 occurring in the Lower and 17 in the Upper
Llandovery; or all but 3 are both Lower and Upper Llandovery ;
and 37 species of Brachiopoda, out of the 109 known, pass to the
Llandovery, 33 of which are Lower Llandovery.
Of the 16 species of Annelida, only 2 pass to the Lower and
Upper Llandovery, Tentaculites anglicus and Cornulites serpularis ;
they range also to the Ludlow.
The class Echinodermata, represented by 32 species, is remark-
able for the occurrence of 8 genera of Cystidea and no less than
23 species. They essentially characterize the Caradoc and Bala
rocks ; with the exception of one species (Hchinospherites arach-
noidea, Forbes), which passes up into the Lower Llandovery, all
are peculiar. Itis only in the Caradoc and Wenlock strata that the
Cystidea are a well-developed and characteristic group of the Kchi-
nodermata; they are replaced in the Carboniferous rocks by the
Blastoidea (Pentremates and Codonaster) and do not appear again.
The Crustacea are the largest and most important class in the
Caradoc. The species number 146, representing 37 genera—Ireland
yielding 90 (the largest number of species), Scotland 78, North
Wales 50, and South Wales 30; or taking North and South Wales
as one area, it has 59 species, 16 genera and 21 species being
common to North and South Wales. Shropshire and Westmoreland
are nearly equal, the former having a known crustacean fauna of
31 species and the latter 35. The genera most largely represented
are Calymene 8 species, Phacops 14, Jilenus 13, Remopleurides 8,
Inchas 6, Stawrocephalus 4, Acidaspis 8, Ampyx 6, Asaphus 6,
Chewurus 6, and Trinucleus 5. The remaining 26 genera (many
of which are Phyllopods) are represented by one or few species.
The 37 genera of Crustacea appear or occur 217 times in the
geographical areas named in the table of distribution and the
horizons they pass to above, and the species appear 433 times.
This Table clearly shows us how much has yet to be done before
we can obtain reliable zoological data, or be assured that the
several classes and genera have been even yet fairly ulustrated,
feeling at the same time that, except by exhaustive and careful col-
lecting, we never shall arrive at even a fair illustration of the fauna
of any given group. For example, the 9 genera of Caradoe Pro-
tozoa are represented by only 10 species, or a fraction more than 1
species for each genus. 8 of these genera belong to the Spongida ;
and only among these do any 4 of the genera, illustrated by 1
ANNIVERSARY ADDRESS OF THE PRESIDENT. 135
Species each, occur in any one locality, as in Shropshire, Scot-
land, and Ireland. North and South Wales have yielded only 2
genera, each with 2 species, in any of the six counties. The
Actinozoa even afford us stronger evidence still of the importance
of specific evidence. In this class we know through the fullest
research that 20 genera and 40 species occur, thus averaging only
2 species for each genus. Many genera (13) have as yet yielded
only 1 species; they are Plasmopora, Syringophyllum, Halysites,
Stylarea, Omphyma, Thecostegites, Alveohites, Aulacophyllum, Calo-
stylis, Cyathophyllum, Pistulipora, Tredadium, and Prosopora. We
cannct suppose for one moment that these genera are not repre-
sented by more species; it is a matter of research only. The
genus Havosites has 8 species, Heliolites 6, Petraia 6, and Monti-
culipora 4. The 20 genera make 90 appearances through the
10 areas, and the species 188; 32 of the generic and 68 of the
specific appearances occur in the formations above the Caradoc,
-and show the relation of one group of strata to another, as deter-
mined through paleontological research. The Lower Llandovery,
which succeeds or is the natural termination of the Caradoc, con-~
tains 9 genera and 20 species of the whole fauna (7°); and the
Upper Llandovery 6 genera and 17 species of the whole. The
coral fauna of the Caradoc at once makes its appearance underived,
the older Llandeilo possessing only 3 species of Actinozoa, Halysites
catenularvus, Favosites fibrosus,and Monticulipora frondosa; whereas,
next to the Wenlock, the Caradoc possesses the largest Coclenterate
fauna of the Lower Palzozcic rocks. Nowhere, either in Europe
or America, does this class appear with so large a generic grouping.
20 of the 40 species pass to. the Lower Llandovery ; most of the
same appear in the overlying and unconformable Upper Llandovery.
The Crustacea pre-eminently characterize the Caradoc and Bala
rocks, and constitute the largest group in the whole of the Palo-
zoic series; 37 genera and 146 species have been collected, de-
scribed, and registered through the labours of the Geological Survey.
of the three countries, England, Ireland, and Scotland, as well as
by the researches of Sedgwick, Salter, M‘Coy, Baily, Sharpe, Prof.
Hughes, &e. No zoological group is better understood, none more
important to the student of stratigraphical geology. The Lower,
Middle, and Upper Bala beds could with difficulty be read or under-
stood without a minute acquaintance with the Trilobita of this vast
middle series of Lower Paleozoic deposits. They are to this group
of rocks what the Ammonitide and Kchinide are to the Mesozoic
series. The order Trilobita is illustrated by 27 genera, the re-
maining 10 are mostly Ostracoda; among them is Z'wrrilepas.
Caernarvonshire has yielded 11 genera and 17 species.
North Denbighshire i ei ee Bow US.
Wales. }) Montgomeryshire id Sie ars) 29s Le
| Merionethshire Fe 1G) a ae DO ee
South f Pembrokeshire % BG S26 24e oe
Wales. { Caermarthenshire Mi DSH § 200 os
12
I 36 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
Rochad Shropshire has yielded 15 genera and 31 species.
Oni ‘etaecie ie ist B86
Scotland as ol ie, 78% ee
Treland ee Silene 90a
The most important genera, or those of chief stratigraphical value
and in which the species are numerous, are Acidaspis (8 species),
Ampyx (6), Agnostus (5), Asaphus (6), Calymene (8), Cheirurus (6),
Homatlonotus (4), Illenus (13), Lachas 6, Phacops (13), and Remo-
pleurides (8). The genera essentially characterizing the Caradoc’are
Harpes, Salteria, Remopleurides, Cyclopyge, Dionide, Trresias, and
Cyphonscus, most of which are only represented by one or few
forms. Scotland and Ireland possess the richest assemblage of species ;
26 genera and 63 species occur in the former, and 23 genera and
77 species in the latter area. Only 15 of the 123 species of Trilo-
bita pass to the Lower Llandovery; they are Acidaspis Brighti,
Calymene Blumenbachu, C. brevicapitata, C. caractacr, C. Allportiana,
Cheirurus bemucronatus, OC. clavifrons, Encrinurus punctatus, Cy-
phaspis megalops, Cybele verrucosa, Illenus Rosenbergi, I. Bowmanni,
I, Thomson, Lichas laxatus, and Phacops Brongnarti. 8 of
these same also pass up into the Upper Llandovery, 6 to the
Wenlock, and 5 to the Ludlow. The long-ranged species are
chiefly those illustrating the largest genera, such as Calymene
Blumenbachui, C. Allportiana, Cheirurus bumucronatus, Encrinurus
punctatus, Cyphaspis megalops, and Phacops caudatus, all of which
species appear in the Ludlow and then cease to exist, the Devo-
nian rocks having none in common; yet Bronteus and Harpes are
repeated from the Caradoc in the Middle Devonian, both in Britain
and on the continent. We must remember, however, that the
marine Devonian nowhere visibly overlies the Silurian rocks in Great
Britain, and the Old Red Sandstone contains no true marine form
anywhere.
The order Ostracoda, illustrated by Beyrichia, Leperditia, Cythere,
Primitia, and Entomzs, needs little more than notice here; they
have received at the hands of Professor Rupert Jones the closest
scrutiny both zoologically, paleontologically, and stratigraphically ;
few men have so largely added to our knowledge of the orders
Ostracoda and Phyllopoda.
Bracutoropa,—And next to the Crustacea in force and classifica-
tory value we must place this group of Mollusca or Molluscoida.
Numerically in the whole of the Cambrian and Silurian rocks the
Crustacea include the largest number of species, 550 being known ;
whilst of the Brachiopoda we know 456. Individually no class sur-
passes the Brachiopoda through all the Palzeozoic and Mesozoic rocks,
many genera being, however, far more richly represented than others.
In the Caradoc this is notably the case. The genus Orthis has in
Britain alone, we know, through the large collections that have been
made and the elaborate researches of Davidson, no less than 110
species, and culminates in the Caradoc. In tracing the numerical
and stratigraphical value of the genus, we find that in the Cambrian
ANNIVERSARY ADDRESS OF THE PRESIDENT. 137
group up to the close of the Tremadoc the genus Orthis possesses
(so far as we know) only 4 species, viz. Or this Hicks, O. Carausi,
O. lenticularis, and O. Menapie; in the Arenig 10 species, the 3
last-named forms being in common with the horizon below; in the
Llandeilo 13 species, 4 of which are Arenig also, viz. Orthis alata,
O. calligramma, O. remota, and O. striatula.
In the Caradoc and Bala group the species have increased to no
less than 41, all having extensive geographical distribution; 7 are
peculiarly Irish. In the Lower Llandovery we know of 20 species,
17 of which are Caradoc, the only 3 peculiar Lower Llandovery
forms being Orthis Bouchardi, O. reversa, and O. mullochensis. Thus
through this one genus alone we see the close alliance of the so-
called Lower Llandovery (the Upper Bala of Sedgwick) with the
Caradoc. The moderate depth at which they lived is clearly indicated
by the coarse and varied arenaceous nature of the deposits, for there
is no evidence to show, even by the zoological grouping, deep-sea
conditions. No Lingule are known in the Lower Llandovery rocks ;
although 6 species occur in the Caradoc and 5 in the Upper Llan-
dovery. The fauna generally may be regarded as one accumulating
under decreasing depth or slow elevation over given areas. 8 of the
20 Lower Llandovery species pass to the Upper Llandovery or May-
Hill beds. To show still further the decline in specific as well as
individual members of the genus Orthis, I may mention that in the
Upper Llandovery there are 10 species, but not a single form
belongs truly to that horizon ; Orthis rustica, the only true Upper
Llandovery species, passes to the Wenlock rocks, so that no form of
Orthis is special to the Upper Llandovery. The species of Orthis in
the Wenlock rocks number 16, of which 8 come from the Llan-
dovery and Caradoc and 4 pass to the Lower Ludlow (Orthis biloba,
O. crassa, O. elegantula, and O. hybrida), so that Orthis Hdgeliana,
Salt., O. Lewrsi, Dav., O. Hughesw, Dav., and O. mullochensis, var.,
or variety of O. reversa, are new and restricted forms. None pass
to the Devonian. I have selected this genus in the Caradoc for com-
parison with the other Silurian groups on account of its magnitude
and stratigraphical value. Two other genera, Leptena and Stropho-
mena, Which first appear in the Llandeilo, also characterize the Cara-
doc by greatly increased specific development. These are Leptena
with 4 species and Strophomena with 2, both individually numerous
in North and South Wales, In the Caradoc Leptena yields 8 species
and Strophomena 19, and for the first time we meet with Rhyncho-
nella with 8 species ; but no form is known to occur in South Wales,
and only 3 have been found in North Wales. Ireland and Scotland
yield 7 of the 8. The following Table shows the specific and stra-
tigraphical value of these four important genera from the Cambrian
to the Upper Silurian :—
138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
E
ie}
7S
=
A :
7
1
a
5
. bo] ob
: 0 5 |
Z qd = S) S tite 6 :
Be 28 dvley Wiese lice. Ise dec Snel
Bes ts |. ae | een en es eo eal
Oe cue bese) 2 le
See ewes koe | =) =
Orthismas ctcuteeelt eee Pe 8) | 14s AY 20s Oe Gs
Heptenarc...oc-cececen| Sec sine Pieepie Nicene cf agin, ta Atle ore eke | mm oe
Strophomena.........] ... ihe 2) .19: |) EE a
Rhynchonella ...... Lh 8.) | BOs eo
O; 1) L| 8] 7 | 21°) 76 | 42 1 (34 aoe
Those genera having only one or two species are doubtless of
equally high stratigraphic significance. Such are Orthisina, Stipho-
notreta, Porambonites, Triplesia, Merista, and Meristella.
LAMELLIBRANCHIATA.—The known species of Bivalvia in the
Caradoc and Bala rocks are more numerous than in any other
Lower Paleozoic group. ‘Thus the Tremadoe rocks of St. David’s
yield to us the earliest Bivalve fauna, consisting of 5 species; the
Arenig has 6, the Llandeilo 6, the Caradoc 76, the Lower Llandovery
only 3, the Upper Llandovery 29, the Wenlock 45, and the Ludlow
71. These numbers help us to see, by comparison, the zoological
value of the class Conchifera in the several strata.
Ctenodonta, Orthonota, Modiolopsis, Pterinea, Ambonychia, and
Palearca are the largest genera, or those: haying the most species,
by comparison with the older and younger‘fortiiations. The Caradoe
Conchifera excel in number all beneath the Carboniferous. The
following Table shows this, through the 6 Caradoc genera above
named :—
B| B
. Bil eS
Sp mo | os
Z 4 = ) 6 i 8 8 ‘
mB | LS a = A S eS a hae =
S last = ls a ra an ee 3
Gos ao | q q < ge esecalere hl |)
ale |e)?|2\s | See eeeecn ee
eens fora) Ss )e <=
Ctenodonta ......... a Dei he Tile Eee 6 3 4
Orthonotay eee loe. MIS | ee 5 1 6 3 | 16
Modiolopsis ......... 4) 1| 2:) 16 | 029) SSc em mes
IPterinvesc ee ere wae Albers | aes 6 1 6) TE we
Ambonychia ......... dae See gee cee SOT eee
iPaleearca, | eeeete mene shies Tae ee 2 a STAR MS 438
<=. "| —_ |J "|_| | || |_| | |__|
4 | 57 2 D1 Dae ares
Cardiola with 3 species, Mytilus with 4, Pleurorhynchus, Ano-
dontopsis, Cucullella, Megalomus, Clidophorus, Arca, and Lyroderma
having each 1 species, complete the Conchifera of the Caradoc. Their
/
ANNIVERSARY ADDRESS OF THE PRESIDENT. 139
geographical distribution is significant, but clearly shows the im-
perfection in collecting, and how much has yet to be done to
demonstrate their relation to the extensive areas over which they
ara distributed :—
Caernarvonshire has yielded 6 genera and 16 species.
Denbighshire a a (RE
Montgomery shire ,, 8 eS 14. —SC««,
Merionethshire __,, 6 “ Los
Pembrokeshire _,, none none
Bo thenskite s 2 i. 2 We
Shropshire ut 5 if TOe ees
Westmoreland 7 3 i Ouhaktss
Scotland a ih R Bye
Ireland ‘5 10 55 Side ee
Nothing short of strict analysis could impress upon us the fact
of such unequal distribution as the above examination shows. No
species of bivalve is known in Pembrokeshire, a district rich in
other groups. Only 1 genus and species in Scotland (Pleurorhyn-
chus dupterus, Salt.), 2 only in Caermarthenshire (Ambonychia triton
and Ctenodonta varicosa, Salt.), and 3 in Westmoreland (Ctenodonta
anglica, D’Orb., Pterinea tenwstriata, M‘Coy, and Cardiola inter-
rupta, Sow.). The physical geography of the area, either through
barren or interrupted coast-line, rather than movements of land or
depth of sea, would most probably account for this unequal distri-
bution and poverty of species in one area, and their comparative
abundance or fair representation in another. Looking at the horizons
which the above 6 genera illustrate, and through which they pass,
it seems hardly explicable that there should be only 3 species of
Lamellibranchiata known in the Lower Llandovery, viz. Pterincea
retroflexa, Mytilus mytilimeris, and Orthonota sulcata ; and these are
Caradoc and Upper Llandovery also, showing us that not a single
species belongs or is confined to the Lower Llandovery. This
result, compared with the large bivalve fauna in the Caradoc or
Lower Bala beds (57 species), and under conformable stratification,
is scarcely to be accounted for, except through elevation of the sea-
bed and change in bathymetrical conditions sufficient, with all
other conditions, to cause the extinction or removal to another area
of the Caradoc Lamellibranchs. Similar results are obtained with
the Gasteropoda; the 53 Caradoc and Bala forms dwindle down to
16 in the Lower Llandovery. The Llandovery species will be noticed
in their place or order subsequently. As before, Ireland yields the
largest number of species (37). .
GastERopopa.—Like the three preceding classes, the group
Gasteropoda is largely represented in the Caradoc strata ; 14 genera
and 53 species have been determined. No species has yet occurred
in Pembrokeshire, and only 3 in Caermarthenshire (Holopella can-
cellata, Sow., Patella saturni, Goldf., and Cyclonema crebristria,
Moy). Neither have we evidence of any species from Westmore-
I40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
land, although, considering the somewhat abundant forms in Shrop-
shire (9) and Scotland (11), and that the Westmoreland area inter-
venes, we might expect some to occur. The genus Huomphalus in
Ireland (with 7 species), Holopewa in Merioneth (7), Murchisonia and
Rhaphistoma in North Wales generally (12), constitute nearly one
half the univalve fauna—T'rochonema, Turbo ?, Trochus?, and Pleu-
rotomaria having but few species in each. 8 genera and 19 species
actually pass up to the succeeding Llandovery, Wenlock, and Ludlow
rocks above. The Lower Llandovery receives 10 species, and the
Upper 16; the Woolhope 1 (Turbo tritorquatus, M‘Coy), the Wen-
lock 2 (EHuomphalus alatus, His., and . sculptus, Sow.). 3 species
range into the Ludlow—Huomphalus alatus, Holopella cancellata, and
H. conica. ‘Three species of Gasteropoda are common to the Llan-
deilo below—Cyclonema crebristria, Murchisoma simplex, and Turbo
tritorquatus. The relationship of the two Llandoveries is marked ;
the Lower has 103 species of all classes in common and the Upper
107, Ireland and Scotland possessing the highest numbers, being re-
spectively 304 and 206.
PrreropopA.—Ten species of this class occur, the largest pelagic
Pteropod fauna known in the Paleozoic rocks ; they occur in nearly
equal numbers through the 10 areas, Ireland still yielding the
highest number, nearly three times as many as Shropshire and
Merioneth. No species is known in Pembrokeshire.
Hetreropopa.—This order is represented in the Caradoc and Bala
rocks by 11 species of Bellerophon, 2 of Kcculiomphalus, and 3 species
of Maclurea. In the British area the two last-named genera are
restricted in their geographical range to Ireland and Scotland, and
stratigraphically to the Arenig or Llandeilo and Caradoc. Maclurea
is known only in Scotland; MM. Logani, Salt., M. Peach, Salt.,
M. macromphala, M‘Coy, and M. magna are said to be (in Scotland)
of Llandeilo age. The Durness species, M. Logam and M. Peachia,
with their associated forms, I believe to be Arenig. Piloceras in-
vaginatum and Orthoceras mendax occur in the same beds. Maclurea
abounds in the Chazy Limestone of the United States and Canada
—hbeds probably to be correlated with our Lowest Llandeilo, the
Upper Cambrian or Lower Bala group of Sedgwick. J. M‘Coyz,
M. macromphala, and M. magna are admitted to be with us of
Caradoc age, and certainly occur low down in the series. Clonmel,
Stinchar river and Bugon &c. in Ayrshire, and the Durness Lime-
stones yleld M. Peachu and M. Logan: abundantly.
I have preferred to place Kcculiomphalus with the Heteropoda
rather than the Pteropoda, although Portlock’s genus may be one
of the latter group.
CrpHatoropA.—No less than 47 species have been determined
from the Caradoc series ; their maximum development is in Ireland,
where 6 genera and 24 species occur; no species is known in Shrop-
shire. Westmoreland and Scotland register 12 each. The Irish
genera are Cyrtoceras, Koleoceras, Lituites, Poterioceras, Trocholites,
and Orthoceras. As a generic fauna this is by far the largest in
ANNIVERSARY ADDRESS OF THE PRESIDENT. I4I
the Paleozoic rocks. Only one species (Orthoceras arcuoliratum,
Hall) is common to the Caradoc and Llandeilo; but 15 species
range upwards—7 to the Lower Llandovery, 9 to the Upper Llan-
dovery, 4 to the Woolhope, 9 to the Wenlock, and 3 to the Ludlow ;
or the 15 make their appearance or occur 32 times in their range
through the higher divisions of the Silurian rocks ; 32 species are
therefore essentially Caradoc or Bala forms. The numerical distri-
bution of the Caradoc species through North and South Wales is re-
markably uniform. 12 species occur in the four North-Welsh coun-
ties, and 8 in the two South-Wales counties. Shropshire possesses
no Cephalopod, yet 57 genera and 1283 species range through 15
zoological classes occurring in that county; but even this number
represents numerically only a little over 2 species for each genus.
Table X. is prepared on geographical data, the universality
or extension of the Caradoc rocks and species not admitting of
any other mode of expressing their distribution; and to analyze
the group under subdivisions of the Caradoc or Bala, as given by
various authors, would end in confusion, owing to the application
of the terms Lower, Middle, and Upper Caradoc, or Bala, not being
the same inall. Text-books have not yet defined the limits of these
divisions, either zoologically or geographically ; in the former sense
the greatest difficulty would be felt over extended areas, through
want of true succession and continuity in strike. A careful study
of the Woodwardian Catalogue demonstrates the difficulty of treating
the Caradoc or Bala group as a whole in any other way. The
column headed ‘ Localities and Numbers” in that Catalogue at once
shows that it is only through space distribution that we can realize
the value of the subdivision. In the Lower Bala group of the Upper
Cambrian, as established by Sedgwick, Mr. Salter has placed 45
genera and 82 species; in the Middle Bala 82 genera and 212
species; and in the Upper Bala group 43 genera and 100 species.
That the fossils of the “‘ Lower Bala” of the Woodwardian Cata-
logue represent the Llandeilo proper of the Geological Survey there
can be no doubt ; and out of the 82 species catalogued, only 17 pass
to the Middle Bala group, and 8 to the Upper Bala. The Middle
Bala of the Cambridge Catalogue receives the fine assemblage of
fossils collected from the Bala limestone, sandstones, and slates of
North Wales, the Caradoc sandstones and the Horderly limestones
of Shropshire, or the true Caradoc. It includes also the fossils of
the Coniston Limestone, the Kildare, Craig-Head, and Peebles Lime-
stones. The Hirnant Limestone is not included in Sedgwick’s
Middle Bala, but constitutes the base of his Upper Bala group. The
212 species largely illustrate the characteristic fauna of the Caradoc,
and the group clearly shows the value of the division (especially
with the elimination of the Llandeilo forms) and its separation
from the Lower Llandovery (the Upper Bala of Sedgwick), into
which only 33 of the 212 species passed. These proportions in the
Cambridge collection (as catalogued), showing the community of
forms between the 3 divisions, show how well the collection was
I42 -PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
made, and also the care bestowed upon the stratigraphical grouping
of the fossils. The Upper Bala group of Sedgwick includes the
Aber-Hirnant Limestone, which occurs above the Bala Limestone,
also the lower part of the Coniston Flags, the beds above the Bala
Limestone, and below the May-Hill Sandstone; it therefore includes
the Lower Llandovery or Mathyraful Limestone near Meifod, and
also the rich fossiliferous series at Haverfordwest, the Dalquorhan
and Mulloch beds of Scotland, and the Maume and Cong beds of
Galway *. The Woodwardian Catalogue enumerates 43 genera and
100 species from this group (the Lower Llandovery of the Geolo-
gical Survey), 18 genera and 36 species of which also occur in the
Middle Bala below.
Lower LLANDOVERY.
In my analysis of the Lower Llandovery species from the rocks
of that age in North and South Wales, Scotland, and Ireland, I have
brought together and tabulated all that is known relative to the
range and distribution of life through this Middle Silurian or Upper
Bala group of Sedgwick. ‘The table shows the value of this upper
member of the Caradoc or Bala beds, and its relation to the transi-
tional Upper Llandovery, or the group so called, which stands be-
tween and connects the Lower Silurian of the Survey with the well-
defined succeeding Wenlock and Ludlow series. Careful analysis of
the species in both their stratigraphical and geographical distri-
bution shows how small a specifically characterized group the Lower
Llandovery appears to be, for only 115 species out of 204 are really
Lower Llandovery. The total number of genera and species known
for all Britain is 68 genera and 204 species; but 50 genera and
104 of these species transgressed or came from the Caradoc and Bala
beds below, thus reducing the actual Llandovery fauna to 18 genera
and 100 species. The intimate connexion with the Upper Llan-
dovery is chiefly through the Actinozoa (20 species), Brachiopoda
(38), Crustacea (10), and Gasteropoda (8). No form of Protozoa,
Echinodermata, or Pteropoda is common to the two Llandoyeries
in any area in Britain.
No species of Echinodermata occurs in North Wales, Ireland, or
Westmoreland. No Lower Llandovery Annelid is known in North
Wales. Neither do we know of any Lamellibranch, Pteropod,
Heteropod, or Cephalopod in the same area. I will now discuss
through tabular analysis the distribution of the chief zoological
groups in the Lower Llandovery, viz. the Echinodermata, the Crus-
tacea, Brachiopoda, and Gasteropoda. The remaining 7 of the 13
groups (there being no plants) are conspicuous through feeble re-
presentation, due doubtless to geographical changes towards the
close of the Caradoc and Bala period.
Hyprozoa.—The careful researches and generalizations of Lin-
narsson in Sweden, Lapworth, Nicholson, Carruthers, and Hopkin-
* Vide Cat. Coll. Cambrian and Silurian Fossils in Mus. Univ. of Cambridge,
pp. 25, 26, 39, & 72, for greater details.
ANNIVERSARY ADDRESS OF THE PRESIDENT.
143
A 2 TE Sm aD ee
=o ee AD 4H won on a 52 mn wo =e | From Llandeilo.
Q bg Q kg
wae ese Soe ee a
[Sect |) 2 Bee Sy See Ess eh ey 3
= Oa a OO AR Eee os
wets 2 Se S Sie eo 6 §
Seo OE o Ss 2 eS SN io
= si «63S fen en erie a of Ee Go £
: Bee 6S. oO: & Se os fo}
: a © - Seale coe J het el laden = ar baa aie ie SS;
: g9 3) OLAS of aCe ge ae =
. wm
2 6 By Qe NARI = algae ail iees eal la R a a
: | 2 SGT SR <p hn dae as enc @
. . . . . oc . . . . . . . . .
: es ops ere ee ea eS
—
~I — et co — — b> bO
Cc aw worroroaoantwnare oo Oo Ke
|
|
|
i | Genera.
Ip
|
|
|
:
~ .
OF | wp oe ee < ao be we Ue be AR BAR AA HE Caernarvonshire.
uo
: iA
‘ ; °
G2 [ow an ue wa sa So oe EY we ca Zo : =~ | Denbighshire. a
5
eg [ee an ae oe Ee So Ta Sy we xe Gx : sw | Montgomeryshire. =
| ss Q
ne =i COS Lec) ARC cole ee : Meri thshir S
aS ai) tm 4P oF LG B& Go AA GX OR > erlonetnsnire. ae
Lar}
OVE &
TM
Sl oe Sr : 5 Ss qo BE AS Fe Bos bop Pembr k hir g E.
EN : 5 a RO wo ~~ : roKkesoaire. = Q
S
| RO rR oe we nm Bo re TO AA ww on wes | Caermarthenshire.| = ae
! | fh Fy
; S
=) ; =
we > oH on oa Da oe we CF AA A® SA AA abo Shropshire. = .
| F | | 8
Se eo ee ee Oe exes, Sm nono) com he W t r i d B
os = pon VS ee ae TS) estmoreland. or
| |
TS an _ ) Ae a9 : De wr
Pegiemo se oF SS ee OH ge OF 2 ae wo aa | Scotland.
| |
se |
oe 2 Of won iS as os aw =i oh 82 oa Pa EN | Treland.
| |
=
og | We He He So we Bo aw 55 ww ww So x» ee | Lower Llandovery.
| |
<A
os | or au we Zo an Yo ow TT ww < : | tipper Manidevary.
| |
Fg
. =
ae | Aw aH fue we iS Ny CQ we an ae Woolhope 2
| | S
an | ow pe wr we To a? bn ©@ Aw fico ne Wenlock.
| |
nS wh Ne Me top ee TO me @r po ah ee Ludlow.
“0PD.WI—'X ATAV I,
144 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
son in Britain, Hall in America, and Barrande in Bohemia, upon
the history, morphology, and distribution of the Rhabdophora
through the Lower Paleozoic rocks of Britain, Europe, and North
America, have greatly added to our knowledge of their stratigraphical
value and distribution both in time and space. To no author, how-
ever, are we so much indebted as to Mr. Lapworth for his exhaustive
researches in this department of Paleontology. Until his careful
analysis and descriptions of the Rhabdophora, as well as the physical
relations, of the Moffat series in Scotland, and his able papers in the
Ann. & Mag. Nat. Hist. ser. 5, vols. i11.-vi., we had little clear know-
ledge either of their zoological grouping or stratigraphical distribution
and relations to other geographical areas, either in Britain, Europe,
or America. That the southern Highlands or uplands of South Scot-
land yield rocks of a peculiar character is well known. They consist
of two types—coarse greywacke, grey, green, or purple in colour,
associated with fissile flagstones, which either alternate with the grey-
wacke, or are arranged separately in zones of considerable thickness.
These two types preponderate. ‘On the west coast, near Girvan,
limestones, shelly sandstenes, and mudstones yield fossils in great
profusion, and both mineralogically and paleeontologically remind us
of the most prolific areas of Wales and Shropshire.”
Certain beds of black carbonaceous shales and mudstones occupy-
ing “long lenticular areas occur in the great mass of barren grey-
wacke; they form extended moniliform lines of great extent, and
range at intervals throughout the northern half of the Southern
Uplands, from the Irish Channel to the North Sea; these black
shales everywhere swarm with Rhabdophora.” It is this group of
Graptolitiferous strata of the south of Scotland (the Moffat series),
and their physical and zoological relations to deposits in other areas,
that Mr. Lapworth has made classical. We know of few or no Lower
or Upper Llandovery Hydrozoa in Wales. The Coniston Mudstones
(Westmoreland) yield 6 genera and 25 species; and these probably
belong to the Lower Llandovery series. The value, however, of the
Scotch deposits, and their Graptolitic fauna of 50 or more species, is
very great; they clearly show us that the paucity of species in
the Welsh rocks is probably due to geographical and other physical
changes.
South of Westmoreland this group had scarcely a representative
after the deposition of the Caradoc, none having survived the close
of the Upper Bala period ; for the Lower Llandovery in North Wales
has yielded few or no species; the Upper Llandovery and the suc-
ceeding Wenlock group, through the Tarannon beds, 5 genera and
23 species ; North Wales 4 genera and 8 species, and South Wales
8 genera and 11 species; Westmoreland 3 genera and 12 species;
Ireland none. These several numbers are as near as I can bring
them, knowing the difficulty of understanding the Llandovery ques-
tion, and omitting in North Wales the sandy or arenaceous Llan-
dovery, which (in that area) does not appear to have furnished a
congenial habitat for the growth and development of the Rhabdo-
phora. Highly favourable, however, the conditions seem to have
ANNIVERSARY ADDRESS OF THE PRESIDENT, 145
been during the formation of the Arenig, Llandeilo, Caradoc, and
Lower Llandovery deposits, as shown in the following table :-—
eREMEOM ee Pee, ee Sse ee 17 genera and 24 species.
MbmmeNOme rie oes Sl 18 e3 44,
JADLLIG | oe ole eee 21 a Srey be
Lower Llandovery of South Wales 5 es ly Guar
Lower Llandovery of Westmoreland 6 cs 20 ee
Lower Llandovery of Scotland... 7 3 Sy bie
Mippersilandoyery .2...-.....- + HE d iage
1 ESET G] Rie ap ge a Re 9 " Zee
_ LUD ab ei eer 3 Be oie Pe
I mention these facts and results here rather than under the
Ludlow section, as the group of the Graptolitide are conspicuous
here, and they are of little value in classification above the Llando-
very rocks. It may be remembered that in 1872* Prof. H. A.
Nicholson published, in the Journal of the Geological Society, a
paper of great originality and highly suggestive of the mode of mi-
gration and distribution of the Graptolites in time and space, or
the vertical and lateral range of this group of fossils. In this paper
Prof. Nicholson endeayours to show the peopling of one area as
derived from another and from points widely separated, showing
that under such circumstances they can never be truly contempo-
raneous. ‘In the present state of our knowledge, however, it must
be more or less provisional and tentative” to attempt to trace the
migrations of any given set of species or groups of fossils; but pro-
bably the time will arrive when definite groups under given conditions
may receive elucidation for lateral range, especially when the original
area of occurrence and dispersion is known. Dr. Nicholson argues,
and justly, that “‘ if we were thoroughly acquainted with the range
of any given fossil or species vertically, and were conversant with
all the details of its geographical distribution, we should then be
able to lay down with some degree of accuracy the lines along which
it must have migrated when the condition of its original area be-
came unsuitable for its further existence therein.” Prof. Nicholson
endeavours to show in his paper certain facts relating to the distri-
bution of the Graptolites, so as to enable us to sketch out the mi-
erations of these and other organisms from their first appearance in
time ; in the case of the Rhabdophora from the Arenig to their final
disappearance at the close of the Ludlow deposits. Five areas are
selected to illustrate the distribution of the Graptolites:—I1st. The
Skiddaw group and its Arenig fauna, as being the earliest in which
the Graptolites appeared, and probably the first area, for we have no
reason to believe that the Canadian or Quebec deposits much preceded
in time our own Cumberland series; the large number of genera
and species not only common to the Skiddaw Slates of the north of
‘England and the Quebec group, but exclusively confined to them,
conclusively and distinctly prove that the area was no small one.
* Quart. Journ. Geol. Soc. vol. xxviii. pp. 217-2382 (1872). “ Migrations of
Graptolites,” by H. A. Nicholson, M.D., D.Sc., &e.
146 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
The differences, indeed, between the Graptolitic faunas of the Skid-
daw and Quebec regions are not greater than what may be due to
imperfect observation, or the effect of difference of station, without
either supposing that one region was peopled by migration from
the other*.
The second area discussed by Dr. Nicholson is that of Wales and
Scotland, containing the Llandeilo Graptolites. The auther believes
that the north of England was dry land during the early portion of
the Llandeilo period, and also that the close of the Skiddaw
(Arenig) period was signalized by the upheaval of the Lake district ;
this, or the unfitness for life of the succeeding seas, in conse-
quence of igneous activity, may have been the cause of no deposits
containing Graptolites being superimposed upon the Skiddaw Slates,
until we reach the higher or later portion of the Caradoc or Bala
period (the Lower Llandovery), at which time an immigration of
Graptolites must have taken place from neighbouring seas. On such
hypotheses, supported by details too minute to discuss here, we may
realize the absence in certain areas of zoological groups whose
existence necessitates the deposition of sedimentary matter con-
genial to their growth and development. Why the Lower and
Upper Llandovery rocks of North and South Wales do not possess a
larger Graptolitic fauna, when in the north of England and Scotland
such a fauna is well developed, can only be explained through
physical changes, either movements of land and sea, or interference
through sedimentary agency, of which there may be many kinds.
Dr. Nicholson further enters into the consideration of the second
great Graptolitic period of the north of England, during which the
mudstones of the Coniston series were deposited. In the Coniston
Limestone proper, which corresponds to the Bala Limestone, no
species have occurred, it being wholly barren of Hydrozoa; but the
so-called Graptolitic mudstones succeeding it abound in species, 6
genera and 25 species having been recorded from them. Many of
these (16) Nicholson believes have been derived from the Upper
Llandeilo of the south of Scotland, the remaining 9 being peculiar
to the Coniston Mudstones. The fourth area Dr. Nicholson calls the
Gala area of the south of Scotland, in Dumfriesshire ; Mr. Lapworth
applied to these deposits the name “Gala Group.” Hight species in
this Gala series are derived from the Upper Llandeilo of the Scotch
area, and the remaining 5 (of the 13) are importations from the
Coniston Mudstones and Coniston area of the Lake district.
The Hudson-River shales and Utica Slates Nicholson believes to
have been peopled by a great migration of the Upper Llandeilo Grap-
tolites of the south of Scotland, which appear to have taken a
westerly course, and ultimately to have reached the United States,
there forming the Graptolitic fauna occurring in the Caradoc or
Hudson-River shales and Utica Slates described by James Hall. |
This view of Nicholson’s, that the Graptolites of the Hudson-River
group are derived through migration from the Upper Llandeilo of the
south of Scotland, he supports or illustrates by means of a table of
* Nicholson, Quart. Journ. Geol. Soe. vol. xxviii. pp. 218, 219.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 147
24 species of Graptolites, 13 of which are so derived. These are
associated with 1 from the Skiddaw and 8 peculiar to the Hudson-
River deposits. Nicholson, in his fifth, or Saxon and Bohemian area,
endeavours to show that two great migrations of Graptolites took
place from the area of the south of Scotland at the close of the Upper
Llandeilo period, one westward through Ireland to America, the other
southward into the north of England; and he suggests a third migra-
tion from the same area in a south-easterly direction, or into the Silu-
rian seas of Saxony and Bohemia. Geinitz, in his “Grauwackenfor-
mation” of Saxony, believed the Graptolitiferous rocks to be the
summit of the Lower Silurian series (Llandovery). Of 5 genera and
12 species given, 4 genera and 10 species are derived from the Upper
Llandeilo of the south of Scotland, and 2 from the Coniston Mud-
stones. Barrande has recognized the British derivation of the Bohe-
mian Graptolites (‘ Défense des Colonies, 1870); he recognizes two
chief Graptolitic zones in Bohemia, viz. Etage D at the summit of
the Lower Silurian series, and Htage E at the base of the Upper.
The Bohemian Graptolites derived from Britain number 5 genera
and 14 species, and are believed to be derived through migration from
the Coniston Mudstones or Upper Llandovery beds of the north of
England. These are identical species with those which lived in the
mudstones named*. I have thus shown that it is only in Scotland
and Cumberland that we obtain a Graptolitic fauna in the Llando-
very rocks (probably Lower), and that none occur in either of the
two Welsh areas‘.
Acrinozoa.—The species of this class in the Lower Llandovery
number a fraction more than 2 to each genus, of which there are 12
(and 26 species). The genera Favosites, Heliolites, and Petrara abound
most in species—Fuvosites 5, Heliolites 4, Petraia6. The distribution
for North Wales is 5 genera and 8 species; for South Wales 8 genera
and 16 species; and for Ireland the same number. Singularly just
as many species pass to the Upper Llandovery (20) as came up from
the Caradoc and Bala beds (20), and in each case 9 of the same
genera; so that in reality the Lower Llandovery rocks possess only
6 species of Actinozoa peculiar to them, so closely allied are the two
formations through this, as through other groups of fossils. 7 of the
9 genera have as yet only yielded 1 species each. Nothing can be
more unsatisfactory than the evidence afforded by such scanty mate-
rials; close research would result in yielding numerous and more
definite species.
EcuinopERmMATA.—No species is known either in North Wales or
Ireland, and two species only in South Wales—Schinospherites
arachnoidea and Glyptocrinus, sp. (stem-ossicles). This last genus
occurs in Scotland also; neither pass to higher formations, but the
same two species occur in the Caradoc.
* Nicholson, loc. cit. pp. 228-230.
+ Recent researches by Lapworth into the specific value and history of the
Rhabdophora have tended to reduce the number of species, great numbers of so-
called species being established on mere fragments of other species. ‘Their
elimination will be of great value to the student of this difficult class of the
animal kingdom.
148 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Crustacea.—The Crustacea of the Lower Llandovery reveal to us
numerically only 2 species in each genus. We have much yet to
learn of the history and zoological relations of the Trilobita of the
Llandovery rocks. The 13 genera and 25 species of this order
mostly characterize the rocks of South Wales and Scotland ; 2 genera
and 4 species only are known in North Wales, Calymene (3) and
Trinucleus (1); and 7 genera and 8 species in South Wales ; Scotland
has 9 genera and 16 species. Eighteen of the Trilobita are also Cara-
doc ; and 8 genera and 10 species pass to the Upper Llandovery ; so
that in the Lower Llandovery one of its largest groups has little
or no stratigraphical value in classification.
Bracutopopa.—This class, like the Crustacea, has little or no classifi-
catory value ; for of the known 10 genera and 59 species in the Lower
Llandovery, 8 genera and 35 species are also Caradoc and Bala, and
10 genera and 38 species pass to the Upper Llandovery. The charac-
teristic species are Meristella subundata, Orthis Bouchardi, Rhyncho-
nella tripartita, Spirifera exporrecta, Strophomena arenacea, Strick-
landima lens, Pentamerus oblongus, and P. undatus. The first ap-
pearance of Pentamerus and Stricklandima is a marked and im-
portant feature in the Lower Llandovery beds. Three species of
Pentamerus (P. oblongus, P. globosus, and P. undatus) are Lower and
Upper Llandovery forms; the 2 species of Stracklandima, S. lens
and S. lirata, are common to both horizons. In North Wales, 8
genera and 22 species occur; and in South Wales 10 genera and 48
species ; Scotland has yielded 8 genera and 29 species, and Ireland
9 genera and 27 species. The South-Wales beds are enriched
chiefly through the genus Orthis with 20 species, Strophomena with
11, and Rhynchonella with 7.
LaMELLIBRANCHIATA.—No species of this extensive group of Mol-
lusca occurs either in North Wales or in Scotland; and we are only
acquainted with 3 genera and 3 species in the Lower Llandovery,
viz. Pterinea retrofleca, Mytilus mytilimeris, and Orthonota suleata ;
these 3 are South-Wales forms, and the Pterinea occurs in the Irish
Llandovery. This meagre representation of so large a class in these
beds, as compared with the Caradoc with 16 genera and 76 species,
clearly shows that at the close of the Caradoc and Bala period great
changes took place with regard to the relations of land andsea. The
Caradoc sea evidently shallowed and reduced its area, and this was
accompanied by corresponding sedimentary changes which governed
the life, habits, and distribution of the succeeding Llandovery fauna.
This is borne out by the Brachiopoda and other groups which
reached such perfection in the Caradoc seas (109 species), Crustacea
(146 species), the Lamellibranchs (76 species), Gasteropoda (53
species), and Cephalopoda (47 species); whereas in the Lower Llan-
dovery many of these groups are scarcely represented ; for example,
the group we are now treating of has only 3 species, the Kchino-
dermata 2, theGasteropoda 16, and the Cephalopoda only 3, with
only 1 species of Pteropod and 1 Heteropod.
Doubtless the strictly arenaceous nature of the deposits and the
somewhat shallow sea constituted the main cause of this extremely
ANNIVERSARY ADDRESS OF THE PRESIDENT. I49
small bivalve fauna. Two of the three species of Conchifera are
Caradoc, and the same two passed to the Upper Llandovery, so that
in reality only | species is to be regarded as Lower Llandovery.
GastERopopaA.—Al]though this class includes a much greater number
of species than the Lamellibranchiata, yet the value of the fauna for
classificatory purposes is equally unsatisfactory. 9 genera and 13
species are known; but of these 6 genera and 10 species are Caradoc
and Bala forms, and 6 genera and 8 species are common to the two
Llandovery series. Only 1 species is known in North Wales (Mur-
chisonia pulchra, M‘Coy), 5 genera and 9 species in South Wales,
and 6 genera with 6 species in Scotland and with 7 in Ireland. Thus
only 6 species of Gasteropoda are truly of Lower Llandovery age—
Murchisona Prycew, M. sulcata, Platyschisma Williamsoni, Acroculia
haliotis, Trochus Moore, and 7’. multitorquatus.
Prrropopa.—The only Pteropod occurring in the Lower Llando-
very is Conularia Sowerby, Det., and this has only appeared in South
Wales and Scotland; none are known in North Wales or Ireland.
This species bridges over the Upper Llandovery, Denbighshire Grits,
and Woolhope series, and reappears in the Wenlock Shales and
Limestones in South Wales and Scotland.
Hzrrrorops.— Bellerophon carinatus, B. bilobatus, and B. dilata-
tus? are the chief Lower Llandovery species. The same 3 are Caradoc,
and B. carinatus and B. bilobatus also occur in the Upper Llando-
very of South Wales and Scotland, B. dilatatus being Irish also.
The species of these two nocturnal and pelagic groups, the Hetero-
poda and Pteropoda, from their habit, had a wide geographical dis-
tribution, and consequently a long range in time also.
CrepHatoropa.— We have seen that the Lower Caradoc and Bala
rocks have yielded no less than 8 genera and 47 species ; the Lower
Llandovery, the highest member of the Bala formation, has, on the
contrary, only 3 genera and 8 species distributed through the 6 areas
in which this formation is represented. The genera are Lituites,
Tretoceras, and Orthoceras. ‘The first-named genus has 2 species,
L. cornu-arietis and L. undosus ; the second (Tretoceras) 1 species,
T. bisiphonatum ; and Orthoceras contains 5 species, O. annulatum,
O. ibex, O. politum, O. tenwistriatum, and O. vagans(?). Of these no
species occurs in North Wales. South Wales, however, in the Llan-
dovery area, has yielded 5 species, Scotland 2 (Orthoceras politum
and O. tenuistriatum), and Ireland 1 species (Orthoceras ibex). Four
of the 8 pass to the Upper Llandovery, and 7 came from the Caradoc.
Tretoceras bisiphonatum and Lituites undosus are the only restricted
Lower Llandovery species out of the 8 known.
The accompanying table shows the complete census of the Lower
Llandovery rocks, and their relationship to the Caradoc below
and the Upper Llandovery above, and at once reveals the fact that
this upper member of the Bala group has no claim to separation
from it; for 50 genera and 105 species unite it with the Caradoc
and Bala proper, and 45 genera and 104 species pass to the
Upper Llandovery ; and we shall find, on casting the life-history of
the Upper Llandovery also, that nearly one half of both genera
VOL, XXXVI. Mm
150 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
and species are also so-called Llandovery; or out of 91 genera and
240 species known in the Upper Llandovery, the above 45 genera
and 104 species occur in the lower group also. Only 16 genera and
101 species are therefore really Lower Llandovery.
Taste X1.—Lower Llandovery.
Geographical Distribution.
S mm eae
S) wa wR ra Oo >
o F i
S Classes. = 4 Sf ao
o Z| 2) S
eS e : = = oc : 6 jts
2. s g a fe = = | Oe
g 2 3 = 5 a & |) aad
= © 8, S 5 8 2 Sai
Fy to) a A D D 5 Ee ia
Plantae ses seteceiee
Fil) LEIROLAOVAOE YS “AU onae mace pane 3 A 3 a
1 5 7 7 6
Ep ||| LelylxoyZory eessabeddser 7 50 A we te & 3
5 ¢ 5 8 7 8
BP || EGBUIVOYACE opodaaoaves 12 26 an A ao oh
2 | Echinodermata...... 2 2 3 E
2 1 9 2 1 1
2) Atameladays tereenee tees 2 3 Be: z iu u 2
10 1D im 4 8 10 7
+ Ore@rustaceaiwscsencees 13 25 P ae 1¢ Z o
AaB RY OZOBiasceemelorec oe 2 5 a 2 z 4 2
8 7 8 10
3 | Brachiopoda ......... 10 59 Bo ae ne a 10
3 | Lamellibranchiata..) 3 3 a Z a 2 2
a 1 6 6
> | Gasteropoda ......... 3) 15 u : 2 5 g
1 | Bteropodarsscvadaces- 1 1 i 1
1 ° 1 a 1
1 | Heteropoda ......... 1 6 3 x 4 2
2 | Cephalopoda ......... 3 8 2 3 1 1
50 22 52 5 4 ;
68 204 43 120 130 98 a5 nice
Uprrer Luanpovery, on May-Hitt Grovp.
Perhaps no formation in the Lower Palseozoic series is more diffi-
cult to understand, either physically or zoologically, than the “ Upper
Llandovery,” or May-Hill group. Its place, stratigraphically, was
long ago settled by Sedgwick, who was the first to point out the
necessity for separating these beds from the Lower Silurian (his
Cambrian), and removed them from the Caradoc in 1853, proposing
the name of the ‘‘ May-Hill Sandstone ” for these beds, being above
all his Cambrian Rocks; and this is so throughout the northern
hemisphere.
On the west flank of the Malverns, at Woolhope, May Hill, and
ANNIVERSARY ADDRESS OF THE PRESIDENT. I51
Tortworth, in many localities in Shropshire (Norbury, Cherbury,
Church Stretton, &c.), and at Llandovery, Presteign, &c. in South
Wales, the Upper Llandovery or May-Hill beds are typically exposed.
Many names have been proposed for these variable beds, such as
Upper Caradoc, Pentamerus-beds, Wenlock Grit, &c.; but, through
their chief development at Llandovery and May Hill, in Gloucester-
shire, the double name of the ‘‘ Upper Llandovery,” or ‘‘ May-Hill
Sandstone,” has been given to them. In North Wales the Upper
Llandovery rocks are absent ; m South Wales they first appear in
Marloes Bay, appearing here and there across Pembrokeshire. Near
Llandeilo, in Caermarthenshire, they lie at the base of the Upper
Silurian rocks, being most variable in thickness. They transgress
or lie indifferently and unconformably on Lower Llandovery, Caradoe,
or Llandeilo beds. In Shropshire they are markedly unconformable
to the Caradoc. In the Longmynd area, under the condition of a
caleareous conglomerate, they rest upon all the older rocks exposed.
That a great physical break takes place between the two Llandoveries
there can be no doubt. They rise from under the Wenlock Shale at
Noeth Grug, strike to near Llandovery and Pen-y-lan; again they
range uninterruptedly from Marloes Bay, in Pembrokeshire, where
they are highly fossiliferous (28 species occurring there), through
Caermarthenshire to Builth, and on to the Longmynd and typical
Silurian country of Shropshire. They everywhere rest unconform-
ably upon the older rocks, sometimes lying on the denuded edges of
the Lower Llandovery or on the Caradoc Sandstone ; at Builth and
the Longmynd on the contorted and denuded Arenig, Llandeilo, and
Cambrian strata.
The absolute unconformity of the Upper Llandovery beds to the
strata below, coupled as it is with changes of species, is doubtless
connected with a lapse of unrepresented time. Whether that time
be of great duration or not we have no means of judging; but,
looking at the intimate connexion between the fauna of the Lower
Llandovery and that of the Upper, we are led to suppose that it
was not of sufficiently long duration to cause either the extinction
or migration of the older fauna or the wmtroduction of a new one
(only 4 genera seem to have appeared); for we have seen that the
Lower Llandovery transmitted 45 genera and 104 species, out of
its fauna of 68 genera and 204 species, to the Upper Llandovery.
It is therefore evident that upheaval and denudation must have
been of comparatively short duration, and little physical change
could have taken place in the area occupied by the Lower Llan-
dovery after upheaval ; this the physical geography and paleontology
of the two groups help to show. |
The preponderance of individuals in species of the genera Pentc-
merus and Stricklandinia, especially P. oblonqus, S. lens, and S. lirata,
which are the best known and most widely spread, is a marked
feature in the Upper Llandovery rocks, and imparts to them peculiar
and distinct facies. These species occur, though not so plentifully,
in the Lower Llandovery. The Malvern and May-Hill form is
S. lens, and it oceurs in profusion. Looking at the grouping of the
m 2
152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Upper Llandovery and the distribution of its fauna, we are surprised
to find that, of the 261 species which occur in the formation, only
136 species really constitute the Upper-Llandovery fauna. The fact
that 104 of the species are Lower Llandovery goes very far to unite
the two so-called formations into one, or a Middle-Silurian group,
abolishing the terms Lower and Upper. Granting the high value of
the unconformity as of paramount stratigraphical importance, yet
the community of fossils and general facies of both horizons lead us
to regard the species as belonging to neither; for certainly the Lower
Llandovery was an expiring close to the Caradoc and Bala, through
elevation of the Caradoc sea-bed, and the Upper through continuity
of certain species ; and the introduction of new forms commenced at
the base of the Upper Silurian of Sir R. Murchison and the Geological
Survey, from which, in the Wenlock rocks, were derived 58 genera
and 125 species; for out of the 523 Wenlock, 125 are Upper Llan-
dovery, 136 species only being the true Upper Llandovery fauna
proper.
Pranta#.—One species only, a fucoid (Pucordes gracilis), is known
in this group of strata. This is probably only one of the many forms
of Annelide or molluscan tracks or burrows, which simulate the
habit of some of the marine alge.
Pror0z0a.—Clathrodiciyon vesiculosum, Nich., and Cliona ( Vioa)
gracilis constitute the only two Protozoa known. The former occurs
in the Llandovery rocks of Scotland; the latter appears to be a
dichotomizing, burrowing sponge, found in the shelly structure
of a Pterincea (P. demissa) from the Upper Llandovery of the Mal-
vern Hills. This is probably the oldest known burrowing sponge ;
its habit is quite that of the modern genus Cliona.
The Welsh Llandovery rocks, although so carefully searched, have
yielded no traces of Spongide. We should, however, quite expect
to find the group Silicipongie, through the Hexactinellide, repre-
sented in these sediments or formations accumulated in moderately
deep water, and associated with an extensive Coelenterate and
Brachiopodal fauna, such as we have in the Upper Llandovery. The
Analytical Table (p. 159) shows that only in two of the ten
(Worcestershire and Scotland) are the Protozoa known.
iypRozoa.—The genera Monograpius, Oyrtograptus, Duplograptus,
and fetiolites alone seem to represent the Rhabdophora in the Upper
Llandovery rocks ; but so many species appear to be common to the
Lower and Upper Llandovery, that it is with difficulty I am enabled
to realize the distinctness of the two faunas. The Irish, Scotch
(Girvan, Gala, and Mulloch beds), and the Coniston flags and mud-
stones have so many species in common with the Lower Llandovery
that only through intimate and practical acquaintance with the two
groups of species can they be separated. In the Valentian or
Llandovery-Tarannon series of Lapworth, including the Birkhil
series and its several zones, so many species of Monograptus, Deplo-
graptus, and Cyrtograptus appear to be common, that it is no easy
task to determine numerically or statigraphically, especially when
geographical distribution is also taken into consideration, their true
ANNIVERSARY ADDRESS OF THE PRESIDENT. 153
history. Probably the Upper Llandovery rocks of Ireland yield 6
or 8 species, the Girvan beds about 30, the Gala group the same, the
Mulloch beds 25 species, and the Coniston beds 25 species; but many
also belong to the Lower Llandovery belowandelsewhere. The species
in two of the genera above named, AMonograptus and Cyrtograptus,
increase in the Wenlock; in which, if we include the species which
occur in the Tarannon Shales lying at the base of the Upper Silurian
(Lower Wenlock group), some 9 genera and 20 species may occur.
As in the Caradoc, it is extremely difficult to arrive at the number
of true species that range through the areas, owing to not having
correct knowledge of the species.
Actinozoa.—This is, zoologically, an important group in the Upper
Llandovery, from the number of genera occurring and the numeri-
eally few species, 11 of the 16 genera being represented only by
1 species each. These are Alveolstes, Coenites (probably one genus),
Halysites, Labechia, Omphyma, Plasmopora, Ptychophyllum, Lind-
stroma, Propora, Pinnacopora, and Streptelasma. Thus only 5
genera constitute a specific fauna, viz. Favosites 4 species, Heliohtes 5,
Paleocyclus 2, Petraia 7, and Syringopora 3. Their dispersion or
distribution is equally significant, showing that the two chief com-
pound genera, Mavosites and Heliolites, are, with one exception
(Peiraia), the most widely distributed geographically. Petraca
occurs in all the 14 localities* ; and perhaps no single genus has so
wide a range or such persistent representative forms, commencing
in the Caradoc with 6 species, having the same number in the
Lower Llandovery, and 7 species in the Upper Llandovery. It is
reduced to 5 in the Wenlock, and 1 (P. bina) in the Lower Ludlow.
We know also of 3, if not 4, Petracw in Lower, Middle, and Upper
Devonian ; they are, however, distinct species, being P. celtica,
Lonsd., P. gigas, M‘Coy, and P. plewradialis, Phil. As regards the
number of genera and species numerically of value, or important
in certain areas, we find that in Pembrokeshire and Cardiganshire
these are but feebly represented. The former county, at Marloes
Bay, has given us 3 genera and 4 species, viz. Mavosites asper,
Omphyma turbinata, Petraia bina, and Petraia subduplicata; and
Cardiganshire only 1, Petraia elongata. Radnorshire has yielded
2 genera and 3 species, Heliolites interstinctus, Petrara elongata,
and P. subduplicata. These few and local species are significant
and suggestive as to the cause of their restricted numbers.
Worcestershire, through the Malvern area, is richest in species, its
7 genera and 18 species being the highest known in the nine areas—
Caermarthenshire and Caernarvonshire having 12, Gloucestershire,
Scotland, and Ireland each 10 species, and South Wales generally 14.
Of the 16 genera and 32 species that range through the Upper Llan-
dovery beds, 14 genera and 22 species pass up into the Wenlock. The
3 genera peculiar to this horizon are Propora (P. Edwardsu), Pina-
copora (P. Anderson), and Lindstromea (L. levis). The remaining
genera and species all pass to the Wenlock series, the Coelenterate
fauna of which numbers 76 species.
* P, subduplicata has recently been discovered in Scotland.
154 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Ecuinopermata.—lt is clearly shown that this group requires to
be more carefully collected and studied. We have 5 genera and 5
species, or only | representative species to each genus. None occur
in Shropshire or Scotland. Two species, representing 2 genera,
have been met with in Pembrokeshire. The species are Actino-
crinus pulcher?, Cyclocystoides Davisu, Salt., Paleaster coronella,
Periechocrinus monliferus, and Paleechinus Phillipsie, Forbes—
the last being the first known representative of the Kchinoidea in
time. The Perischoechinide, to which family this genus belongs,
attained its maximum development during the Carboniferous
period, both in Britain and America. No fewer than 7 genera
have been recognized in America and 4 in Britain. In the test
of Paleechinus the interambulacral plates abut against each other,
not being bevelled for overlapping articulation, as is the case with
Perischodomus, Oligophorus, Melonites, and other genera. The family
Archeocidaridee, of which the Carboniferous genus Archwocidaris 1s
the type, does not occur below the Carboniferous rocks in any known
area. The modern representative, ‘‘ Calveria” (C. hystrix) of Prof.
W. Thomson, has been dredged in 445 fathoms water (2670 feet) in
lat. 59° 38’ N., long. 7° 46’ W. Calveria differs from all known
recent Kchinoidea through the structure of the plates of the test,
which overlap, instead of abutting against each other, as in all other
genera. Again, the plates composing the interambulacral areas over-
lap from the apical disk towards the mouth, and those of the ambu-
lacral area from the mouth towards the apical disk, or in the reverse
direction. This ancient type appears in the Chalk as Echinothuria
(E. floriformis); and now, through the dredgings of the ‘ Porcupine,’
we have proof of ifs continuity from the Cretaceous epoch.
AnnrLIpA.—Three genera, with four species, two of which claim
attention here, viz. Ventaculites (ornatus, Sow.), and Cornulites (serpu-
laria, Schloth.). They have occurred in almost every locality since
their first appearance in the Caradoc and Bala beds. Tentaculites
ranges through the Caradoc everywhere except in Scotland ; it is
abundant in the Lower Llandovery of South Wales; but its maxi-
mum of development takes place in the May-Hill Sandstones, where
it is a marked feature in the fauna. It is sparingly exhibited in the
Wenlock shales and sandstones, Cornulites having replaced it indi-
vidually in those beds. TYentaculites anglicus, T. ornatus, and
7’. tenwis are also Ludlow species; and the long-lived 7. anglicus
either passes to the Middle Devonian slightly modified, or is replaced ~
by Schlotheim’s species 7’, scalaris.
The 3 genera and 4 species (Cornulites serpularius, Tentaculrtes
anglicus, T. ornatus, and Spirorbis Lewis) pass to the Wenlock.
The Cephalobranchiate or Tubicolar Annulosa (Annelida) play an
important part in the life and distribution of the class through
time. Their habits insure persistency, their structure security, and
their bathymetrical ranges are such as to lessen their chances of
modification through relative changes of land and sea. No form of
the order Errantia, or Dorsibranchiate Annelida, has been detected
in the Llandovery rocks, although, doubtless, they existed, as many
ANNIVERSARY ADDRESS OF THE PRESIDENT. 155 .
of the so-called fucoidal remains are only tracks of these creatures ;
and their presence has been demonstrated by Mr. G. J. Hinde
through his discovery of the jaws of many species of the Poly-
cheta in the Silurian, Devonian, and Carboniferous formations.
In the Wenlock alone he has discovered the remains of 6 genera
and 24 species; and in the Ludlow 2 of the same genera and 6
species. No one can doubt that, by careful sifting and preparation,
the clays and shales of the still older rocks may yield a rich harvest
of the remains of the Annulosa and soft-skinned Echinoderms. This
process is now bearing fruit through the energetic measures em-
ployed by Mr. G. Maw, in having large quantities of the Wenlock
Shales washed, sifted, and examined. Numbers of new forms have
been discovered. The same result has been obtained through the
determined and persistent search made by Mr. Bennie (the Collector
for the Scotch Survey) for remains of the Holothuride in the Car-
boniferous shales of Scotland, and also for the Chitonide. ‘The
results obtained by this patient worker, and the species collected, are
now being described and figured for the Glasgow Geological Society
by Mr. Etheridge, Junior.
It is now the age of microscopical investigations, and ere long
microscopic paleontology will stand on the same footing with petro-
logical and crystallographic investigations.
Crustacea.—The distribution of some of the species of the Crus-
tacea through the Lower Llandovery is more constant and uni-
versal than in any other Silurian deposit. Calymene Blumenbachu,
Eincrinurus punctatus, Ilenus Thomsom, Proétus Stokesw, and Pha-
cops Stokesi occur in almost every locality, and all 5 pass to the Wen-
lock. 7 of the known 24 species do not pass to any higher horizon than
Upper Llandovery; they are Illenus emuius, I. Bowmanm, I. Mac-
callunn, Phacops Weaveri, P. obtusicaudatus, Lichas laxatus, and Tri-
nucleus concentricus. .'To show how equally the species are distri-
buted, I may state that in Caermarthenshire 7 genera and 12 species
occur ; in Pembrokeshire 7 genera and 11 species ; in Worcestershire
7 genera and 13 species ; in Shropshire 7 genera and 15 species; and
in Ireland 7 genera and 14 species; and, singularly also, 7 genera and
14 species pass to the Wenlock. As we have before seen, 10 species
are Lower Llandovery and Caradoc—thus, as regards the Crustacea,
rendering the value of the Upper Llandovery as a distinct paleon-
tological group more questionable still.
Bracuiopopa.—tThe species in this class are more than double the
number of those of any other in the Upper Llandovery rocks. We
recognize 65 species and 13 genera. The geographical distribution
of Atrypa (5 species), Leptena (4), Orthis (10), Pentamerus (4),
fihynchonella (9), Stricklandinia (2), Spirifera (5), and Strophomena
(11) is complete through South Wales, Gloucestershire, Worcester-
shire, and Shropshire. These 8 genera include the mass of species
(50 of the 65) that range through the fourteen localities I have
selected, and whence I have drawn the materials for analysis, and
I believe I have omitted none. Lingula with 5 species, Crania and
Discona each with 1, Chonetes with 3, and Meristella with 6 species
156 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
are sparingly and irregularly distributed ; but we should expect this
from the habits and habitats of 3 at least of the genera. No less
than 36 species come up from the Lower Llandovery (22 of the same
are Caradoc); and 41 of the 65 range into the Wenlock beds. As
among the Crustacea, few species belong to the Upper Llandovery
proper, showing how slight is the evidence afforded us to separate the
Lower and Upper Llandovery. The stratigraphical unconformity is,
however, completely borne out by a corresponding paleontological
break. This is most decisively seen from the Actinozoa, the
Crustacea, the Brachiopoda, and the Lamellibranchiata; indeed Car-
diganshire has as yet only yielded | species of Actinozoa, Petraia
elongata, M‘Coy. The Upper Llandovery rocks of the nine chief
areas given below have yielded the following number of genera and
species of Brachiopoda :—
Counties. Genera. Species.
Remibrokeshines 7.40 ae. 11 19
Caermarthenshire ........ a, 38
Cardiganshirenc. seen oe none. none,
IRGOGESOS So esessacece 6 De
Gloucestershire .........-. 9 it
Wrorcestershires 4 ae att 35
Shmopsiune yeti ae ae 13 13
SCOGlAMGs 2s cc ct ee aiee mee 9 De,
Terelamndiy: case ee eo oun 10 19
No less than 11 genera and 41 species pass up to the Wenlock
group, thus showing that a greater number of species in this class
pass up than belong to any even of the most prolific areas.
LAMELLIBRANCHIATA.—Considering the few species known in the
Lower Llandovery (3), we have here a marked change in the greatly
increased fauna of bivalve Mollusca, which have increased from
the 3 genera and 3 species of the Lower Llandovery (Pterincea retro-
flexa, Mytilus mytilimeris, and Orthonota sulcata) to 12 genera and
29 species. 2 of the 3 species above named pass to these upper beds,
so that the specific fauna is essentially new; in the end, however,
it gives to the Wenlock 7 genera and 15 species; or 50 per cent.
pass to the Wenlock. The Worcestershire area is most prolific,
12 species occurring. Only 3 species are known in Scotland,
Anodontopsis bulla, Pterinea Sowerbyt, and Cardiola striata, and 3
in Ireland, Anodontopsis bulla, M‘Coy, Pterinwa bullata, M‘Coy,
and Ctenodonta subcylindrica, M‘Coy. No species is known either
in Radnorshire or Caermarthenshire. (Vide Table No. XII.)
GastEropops.—Kqually balanced with the above group, the dis-
tributional value being through species of Holopella, Acroculia, ha-
plistoma, and Turbo. These species, too, have a wide geographical
distribution, Worcestershire, as before, possessing the greatest num-
ber of species (9), although here only equal to Ireland, which has
also 9 species; while Caermarthenshire has 7, the remainder of
the 13 genera and 28 species being equally distributed. 6 genera
and 8 species pass to the Wenlock; they are Acroculia halts,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 157
Euomphalus alatus, E. frenatus, E. sculptus, Holopella obsoleta,
Loxonema sinuosum, Murchisonia articulata, and Turbo tritorquatus.
No form occurs in the Upper Llandovery of Cardiganshire.
Preropops.—Only | species is known in the Upper Llandovery.
Conularia cancellata, Sandb., occurs in Gloucestershire and Shrop-
shire, and is known in no other formations or localities in Britain.
The more abundant C. Sowerbyi is Lower Llandovery, Wenlock,
and Ludlow. It is questionable if C. cancellata is really a British
species or only a variety of C. Sowerbyt. 7 of the 10 areas have
no represesentative of this group.
Herzroropa.—Leculiomphalus (Cyrtolites) and Bellerophon, the
. former having 2 species (#. levis, Sby., and £. scoticus), the latter
9, range pretty equally through the Upper Llandovery rocks,
B. dilatatus, B. trilobatus, and B. carinatus haying the widest or
most extended geographical distribution. The rarer forms, Hecul-
omphalus scoticus, M‘Coy, Bellerophon subdecussatus, M‘Coy, B. wen-
lockensis and B. obtectus, Phill., have as yet only occurred each in
one locality ; 5 of the 11 have appeared before in the Caradoc; but
only one species, B. carinatus, seems to have been Lower Llandovery.
These Pelagic Mollusca, especially the family Atlantide, have no fixed
habitat, their distribution being quite independent of the nature of
the sea-bottom, so that the Bellerophons of the Silurian, Devonian,
and Carboniferous periods occur indifferently in mechanical deposits
of the most varied petrological or lithological characters. The great
Poreellia (P. Woodwardit, Sby.) of the Middle Devonian, or the two
species P. striata and P. Symondsii of Phillips, occur in all sorts of
deposits all through the history of the genus, of which 12 or 14
species range from the Devonian to the Trias, Belgium having
afforded many forms. Conrad’s genus Cyriolites, probably the
Ecculiomphalus of Buckland, is represented in Britain by 3 species
—H. Bucklandi, Caradoc only; £. levis, Upper Llandovery, Wen-
lock, and Ludlow; and Z. scoticus, Llandeilo, Caradoc, and Upper
Llandovery. Of the 11 Upper Llandovery species 6 pass to the Wen-
lock, 5 being species of Bellerophon, and 1 Eeculiomphalus (EL. levis).
CrpHatopopa.—Of the 6 genera occurring in the Upper Llan-
dovery, viz. Actinoceras, Cyrtoceras, Lituites, Phragmoceras, Treto-
ceras, and Orthocerus, one (Actinoceras nummularium) appears for
the first time, and the rare forms Phragmoceras compressum and
Cyrtoceras upproximatum have but local geographical distribution.
The last named is from the Upper Llandovery of Malvern only;
P. compressum the same, being of doubtful occurrence in the Ludlow
rocks. We have seen that the Caradoc rocks of Shropshire have not
yielded a single species of Cephalopod; but here, in the Upper Llan-
dovery of the same county, we have 3 genera and 9 species; yet 8
genera and 47 species occur in the Caradoc rocks. This fact, coupled
with others to be arrived at through the tables of distribution,
tends to show the shallowing of the Caradoc sea and slow elevation
of the land through the latter part of the Caradoc period, and the
time represented by the deposition of both the Lower and Upper
158 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Llandovery series. 4 genera and 9 species pass to the Wenlock.
Ireland has only 2, Orthoceras coralliforme, M‘Coy, and O. subgre-
garium, M‘Coy. Radnorshire has 1 species, Litwites cornu-arietis,
Sow. Taking South Wales generally, only 6 species are known
there, and these represent 4 genera—Actinoceras 1 species, Lituites
1 species, Orthoceras 3 species, and T'retoceras 1 species.
The Upper Llandovery rocks of Scotland give us 4 species,
3 Orthocerata and 1 Phragmoceras (P. compressum),.
We therefore find that, out of the whole fauna of the Upper
Llandovery rocks, numbering 240 species, only 91 are confined to
them and do not pass up. The following list shows the special
Upper Llandovery fauna :— i“
RObOZ08) 44 Weinents ee 2 species.
iNctamOzoa,! Joe aa are. Ae 10 “3
Kehinodermata.......... 3 a
Crustacea vik ae. ee 8 ee
TTY OZ OA cphisual.-p senses net eenae evel igs
Brachiopodarn es -.ntiee ee 22a ae
Lamellibranchiata ...... 11 Be
Gasteropoda)j2 OV isin kek ening
Pteropodas. secigisiat wick & il: <
Meteropodauc...u ee. aes RO ee
Cephalopoda ss. er Dit.) U5
i
WENLOCK.
I have stated that 58 genera and 125 species are common to the
Wenlock rocks and the Upper Llandovery; in other words, these
125 species pass up from the Llandovery to the Wenlock formation.
Next to the Caradoc and Bala, the Wenlock group, embracing the
Tarannon Shales, Denbighshire Grits, and Woolhope beds, possesses
the largest Silurian fauna known; it numbers 168 genera and 530
species. Hight chief groups or classes out of the fourteen furnish the
majority of the species, in each case attaining their maximum in the
Wenlock Limestone. ‘They are the following :—
said now oa yi ats ees 6 genera and 30 species.
2s Achimozoa nts dea a 25 45 ROr es
3. Echinodermata ...... 28 genera and 68 species.
4: Orustacealys)) 28). 210.8 27 3 Vestn Ones
oi) brachiopodaniee ase 21 F Oss ees
6. Lamellibranchiata .... 16 He AB yk
Ge (Gasveropoda (ia. s en: 9 : PATRIA
&. Cephalopoda =) .. 78 5 y DOT es
I may add the Bryozoa, for at no period in the history of the
159
THE PRESIDENT.
S OF
ES
SARY ADDR
ANNIVER
Taare XII.— Upper Llandovery.
Geographical Distribution.
net
= o i
w o Pat ot ats) P:
i re q a a | 4 ae ass
Se Classes. a g a = S g a g Os to
oir : \ ng :: A rz 2 a =) 08 ag rd Wenlock.
wb) 3 n ia &o Oo a4 o © n m 5 a
o
ES Ce Wee en coh ge erate eegin Sh calgon er enemas
Sg | 3 Ee 3 = ae: = 3 3 be i= 5
es B) a, ) @ @ S A oa! te ae So co)
By a) MD or Oo o) ete wn O A) HO RQ
Plone atcmamectsrakealt acl 1 oa 6 oe : 1
EOUOZO 8 ax the ates catewete, 2 UE) Vee a vee ves wee ves te 1 “ vee i
Heled |) HAV GIOZOA:. vac hes ccavtevcescule — 4 33 *F ... on ie ve tee oe nee vee 2's 30
9 : " 3 5 3 10 6 7 4 7
a0 UNGEINOZOBN. cate: A ctor oul RHO 32 4 12 i 3 14 10 18 9 10 22
Eechinodermata..............., 5 i) 5 vee oC 1 5 I 2 vee 2
/NOIMIOES coemaooddgecorcodecon|=. & 4 3 “ ves 1 3 3 3 3 vee ' 4
8 7 7 6 7 6 7 7 6
a Onustacode. ncn all Pie || art 13 : 8 13 & 13 15 vee 7 14
2 . é N 2 2 BY 1 1 1 <
2 BUYOZOS ayaacnaieesianescsecl 2 7 vee 3 vee ves 4 3 1 2 : 1 3
10 . 7 tC 11 6 9 11 13
PU EMECHIONOCay ins. cme: LG 65 Ae an im As ate 27 35 13 000) 12 44
2 Lamellibranchiata .........) 12 29 7 4 vee see 3 8 2 é ee 1 15
6 : ‘ 4 3 9 3 4 4 3 ;
g 1) Grasteropoda...c.c.e.0 LO 28 3 7 3 11 é 9 5 nee 4 8
UREGHOMOG Esta dew. tevteenccw cs 1\ Tit exe fo BEC Guie ade A eee i
2 1 1 1 1 1 1 1 1 2
? Re terO pode. .ce.cmeacnnl wee Hel IY PE i . 1 3 1 3 7 os 4 6
1 | Cephalopoda ...... cenceualh Ome ie Ong 4 aa 1 é : 3 ve 4 9
A5 38 42 22 54 41 48 41 6 35 59
104 thse eeeeees 91 261 H 658 90 I 40 106 70 VOR ke 25 74 126
|
i ae iS a 2) eS Np I Sa Le lA Nhe al ee ee al eee eel ee ARR ge
* It is difficult to decide with regard to these species which are Upper and which Lower Llandovery.
t L also give these 6 genera and 25 species in the Upper Llandovery as well as the Lower, for I really know not whose view to adopt as to their
stratigraphical position, Mr, Avyeline and Prof, Hughes place them in the Tarannon Shales, Mr. Lapworth and Dr. Nicholson in the
Lower Llandovery.
160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Lower Paleozoic rocks were they so largely represented, and all the
known forms in the Wenlock group (11 genera and 24 species)
occur in the Wenlock Limestone and Shale, and in those of England
alone, only 1 species occurring either in Scotland or Ireland.
Protozoa.—Chona prisca and Spongarium Hdwardsii are both
Denbighshire-grit species, the latter being also Wenlock and Lud-
low; Cnemidium tenue occurs in the Wenlock only, and Ischadites
Grindrodi in the Woolhope; the other well-known species, J.
Keng, Murch., has a wider range both in time and space, and has
occurred in the Wenlock rocks beneath the Cretaceous series at
Ware, in Herefordshire, in the Silurian cores brought up from a
depth of 1000 feet, during trials for the better supply of London
with water. 30 Wenlock species were obtained here from a few
feet of cores; they are identical with the Wenlock species of Dudley
and Wenlock Edge. (Vide page 229, in the Chapter upon the
extension of the older rocks under the London area.) The singular
and still doubtful genus Stromatopora (NS. striatella) occurs plentifully
in the shales and limestones of the true Wenlock beds, and is also
found in the Aymestry Limestone. This genus comprises a large
number of Silurian and Devonian fossils of every size and form. The
affinity of the Stromatoporids is still doubtful; by some authors they
are placed with the Hydrozoa, in the subclass ‘“‘ Hydrocorallina.”
The doubtful Devonian genus Caunopora suggests much research,
both from its abundance and peculiar structure. In Britain Stroma-
topora first appears in the Caradoc and Bala group, ranging upwards
into the Middle Devonian of Devonshire.
Hyprozoa.—The Wenlock rocks (assuming the Tarannon and
Denbighshire beds to be at their base) have yielded 6 genera and 30
species. Stratigraphically they occur chiefly in the Tarannon beds,
or probably the Denbighshire Grits. So far as | know there are
none in the Woolhope beds, and I omit them from the column
headed Wenlock, as they occur chiefly at Builth and in North Wales,
and in this case would be repeated. The T'arannon or Denbighshire
beds have yielded 5 genera and 23 species; North Wales 1 genus
(Monograptus) and 8 species; South Wales 3 genera and 15 species ;
Westmoreland 3 genera and 16 species; Scotland 3 genera and 5
species.
Acrinozoa.—At no period during the progress of Palseozoic time
was there so large and rich a Coralliferous fauna as during the
Wenlock period; numerically the Middle Devonian about equalled
the Wenlock species in number, the genera and species being in both
deposits much the same. The Wenlock rocks of Britain yield 25
genera and 76 species, the Devonian 24 genera and 52 species,
and the Carboniferous 36 genera and 141 species.
I believe every known Wenlock species (there are 76 of them)
occurs in the Wenlock Limestone and its subordinate shales. In the
lower division, especially the Tarannon Shale and the Denbighshire
Grits, the species are few, not more than five being known in the
former and four in the latter.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 161
The Tarannon species are Havosites asper, I’. fibrosus, F. gothlan-
dicus, Petrara bona, and P. subduplicata. The four Denbighshire-grit
species are also Favosites aspera and I’. fibrosus, Petraia subduplicata
and Syringopora serpens. The upper member of the Lower Wenlock
(the Woolhope beds) yields 16 genera and 26 species, most equally
distributed generically. The North-Welsh Wenlocks yield 7 genera
and 11 species, and the South-Wales beds 10 genera and 18
species ; Scotland 8 genera and 11 species; and Ireland 14 genera
and 23 species.
We must not forget that 14 genera and 22 species came from the
Llandovery rocks, and 18 pass to the Ludlow group, 13 of which
were also Llandovery ; thus 41 species are peculiarly Wenlock.
Ecutnoprermata.—As compared with the Upper Llandovery, with
only 5 genera and 5 species, and the Lower Llandovery only 2
species, the Wenlock sea must have been highly favourable to the
development of the Echinodermata ; no greater development of life
is known in any formation, for 60 of the 68 known species of
Echinodermata were new appearances in the British area. Many
are American ; 65 of the 68 are Wenlock Limestone; no species is
known in Scotland, and only 1 in Ireland (Acéenocrinus Wynne,
Baily); only 1 species occurs in N. Wales in the Tarannon Shale
(Actinocrinus pulcher), and only 2 in the Woolhope (Lucalyptocrinus
polydactylus, M‘Coy, and Pisocrinus pilula, De Kon.).
We should expect that out of so large a fauna many species would
pass to the higher divisions of the Upper Silurian, but only 4 genera
and 6 species pass to the Lower Ludlow. These are of the Crinoidea,
Actinocrinus pulcher, Ichthyocrinus pyriformis, and Ichthyocrinus
M‘Coyanus ; of the Cystidea, Pseudocrinites magnificus, P. quadrifas-
ciatus; and of the Asteroidea, Rhophalocoma pyrotechnica. Ichthyo-
crinus pyriformis is the only species occurring in the Aymestry
Limestone ; the Upper Ludlow only holds 1 species in common with
the Wenlock, the long-lived Actinocrinus pulcher. No less than 20
new Kchinodermal genera made their appearance in the Wenlock
sea, and 17 of them are confined to the Wenlock rocks; the 4 genera
that pass to the Ludlow are Ichthyocrinus, Taxocrinus, Pseudocri-
nites, and fhophalocoma. ‘This marked, sudden, and important
addition to the 3 orders of the Echinodermata can only be explained
upon the theory of migration from some prolific area; whence it is
most difficult to suggest ; but looking at the great generic and specific
development of the Crinoidea, Cystidea, &c. in N. America, and
the great resemblance, if not identity, of the faunas in the two
areas, would lead one to surmise that it was from the west rather
than from Europe that the Wenlock sea derived these HKchino-
dermata.
Awnetipa.—No other British Palxozoic strata possess so many
species of Annelida; they number 35. The Upper Llandovery
possesses only 4 species, the Lower Llandovery 3, the Caradoc 16,
the Llandeilo 3, and Ludlow 17 species.
This exuberance in the Wenlock strata is due to the researches of
162 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
one naturalist *, through whose careful investigations no less than 6
new genera and 24 new species have been added to the Annelidan
group of the Wenlock. We know of but one Wenlock species in
Scotland or Ireland. All except one species occurs in the true
Wenlock Limestone and shales: 4 species pass to the Lower Ludlow
(Helminthites, sp., Serpulites dispar, S. longissemus, and Sprrorbis
Lewis) and 8 to the Upper (viz. Cornulites serpularius, Serpulites
dispar, S. longissimus, Tentaculites anglicus, T’. ornatus, Tr ach yderma
squamosa, and 2 species of Arabellies).
CrustacEA.—Ten new genera appear here for the first time; it is
important to name them—Turri lepas, Aichmina, Cyphaspis, Deiphon,
Eurypterus, Hemiaspis, Pterygotus, Thlipsura, Cythere, and Cythe-
rellina. 'The entire Crustacean fauna consists of 27 genera and 78
species; the Upper Llandovery transmits to it 7 genera and 14
species: 74 of the 78 species occur in the Wenlock Limestone ; and the
4 wanting species are Homalonotus cylindricus, Ceratiocaris ludensis,
Primitia excavata, and P. lenticularis. The Woolhope beds hold a
remarkable Crustacean fauna, comprising 13 genera and 24 species :
this class and the Brachiopoda are the only two marked zoological
groups in this division of the Lower Wenlock series ; 12 of the Trilo-
bita are Upper Llandovery, and only 1 is distinctly a Woolhope
species, viz. Homalonotus cylindricus, Salt. The remaining 3 species
of Crustacea in the Woolhope are Primitia excavata, P. lenticularis,
and Cythere Grindrodiana, Salt., all belonging to the Ostracoda ;
they are of no value. We thus rather unexpectedly find that the
Woolhope formation possesses groups of fossils almost equal to
those of the Wenlock Limestone; such as the Actinozoa with 26
species, 18 of which are also Upper Llandovery; the Crustacea
with 24 species, 19 of which are Trilobites; the Brachiopoda
with 17 genera and 56 species out of the 21 genera and 96 species
known in the Wenlock Limestone. The poverty of the Crustacea
in the Tarannon and Denbighshire Grits might be expected from the
lithological characters of the rocks; only 8 of the 78 species occur
in the former, and 5 in the latter horizon. North Wales has only
yielded 5 genera and 11 species, and South Wales 9 genera and 14
species ; only 3 species occur in Scotland—Turrilepas Wirightianus,
Beyrichia Kleedeni, and Phacops Stokes. 'The Irish species number
8—Calymene Blumenbachit, var. Allportiana, Cheirurus bimucronatus,
fnerinurus punctatus, EL. variolaris, Phacops caudatus, P. nudus, P.
Stokesti, and Proétus latifrons. The order Merostomata makes its
first appearance in the Wenlock through Hurypierus punctatus,
flemiaspis horridus, and Pterygotus problematicus, all in the Wenlock-
Limestone series. This group of Crustacea has been extensively
and critically worked out and illustrated in a masterly manner
by Dr. H. Woodward, F.R.S., in the volumes of the Palzonto-
graphical Society, the Quarterly Journal of the Geological Society,
and the ‘Geological Magazine.’ The suborder Eury pterida i is repre-
* G. J. Hinde, Quart. Journ. Geol. Soc. vol. xxxvi. pp. 368-378.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 163
sented by 5 genera, 3 of which commence or first appear in this
division of the Upper Silurian strata. No less than 12 species of
Primitia, besides other Ostracods, have been determined by Prof.
Rupert Jones, F.R.S., two of them being Woolhope (Cythere Grin-
drodiana and Primitia lenticularis). Of the whole group of Crus-
tacea, 13 genera and 18 species pass up to the Lower Ludlow, whose
Crustacean fauna numbers 18 genera and 47 species.
Bryozoa.—Of the 11 known genera that occur, 6 are new in
the Wenlock. No less than 24 species are known in the shales
and limestones; none have occurred in the Tarannon Shales, Den-
bighshire Grits, or anywhere in North Wales or Scotland. In South
Wales 2 species are known, Drastopora consimilis, Lonsd., and Péilo-
dictya lanceolata; the same species occur in Ireland, and, with Escha-
rina angularis, Lonsd., pass to the Lower Ludlow. Fenestella
assimilis, F. subantiqua, and Ptilodictya lanceolata were also Lower
Llandovery species. The 6 genera not known in the older rocks,
and which first appear in the Wenlock, are Cellepora, Ceriopora,
Diastopora, Discopora, Hscharina, and Polypora.
Most of the Paleozoic genera belong to the order Gymnolemata,
suborder Cyclostomata. We know of no Paleozoic genera extending
into the Secondary Period, where this class attains its maximum
paleontological development, the Cretaceous system alone having
yielded more than 200 species.
BracwropopA.—In the Wenlock rocks, like the Caradoc, the Bra-
chiopoda greatly predominate over most of the other groups. We
have determined 15 genera and 109 species in the Caradoc; and now
in the Wenlock are enabled to show that 22 genera and 101 species
occur, being an increase of 7 new genera (namely, Athyiis, Cyrtia,
Fiichwaldia, Nucleospira, Obolus, Orbiculoidea, and Retzia), the species
being fewer so far as we know through the literature of the class.
21 genera and 96 of the 101 species belong to the Upper Wenlock
or Wenlock Limestone and shale*; all the known 22 genera are
also represented in the same horizon. The Woolhope beds yield 17
genera and 56 species, every Woolhope shell being also Wenlock.
Orthis mullochensis, Dav., or its variety O. reversa, may stand alone
as a Woolhope species, but every other form is equally Wenlock.
Certain horizons in the Wenlock rocks are richer generically and
poorer in species than others; this is shown in the Tarannon Shales
and Denbighshire Grits, where, in the former, 10 genera occur
with only 15 species; it is the same with the Denbighshire Grits,
in which we have 14 genera and only 19 species. No genus or
species is peculiar to either the Tarannon or Denbighshire beds;
all are good Upper Wenlock forms. ‘Those species having the
longest range in time in the Wenlock group number about 11; they
also have a correspondingly wide range in space; they are :—
* The researches of Mr. Davidson, F.R.S., upon the collection made by
Mr. G. Maw in these beds has enabled him to add many new species and one
or two new genera to the fauna of the Wenlock rocks.
164 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Atrypa reticulata.
Rhynchonella nucula.
Chonetes striatellus.
Spirifera elevata.
Crania implicata. exporrecta.
Leptzena transversalis. Strophomena pecten.
Meristella tumida. rhomboidalis.
Orthis elegantula.
All those named have appeared in the Llandovery or Caradoc
before, and all pass to the Ludlow; but their universality through
the Wenlock renders them conspicuous or long-lived, though not
perhaps the best witnesses in determining the age of any particular
horizon through the Wenlock deposits; those species which are
short-ranged, or essentially typical or confined to particular beds,
should be named, as contradistinguished from those given above.
No species is peculiar to the Tarannon Shale, although 10 genera
and 15 species range through this series of beds. No species essen-
tially marks, distinguishes, or is confined to the Denbighshire Grits ;
yet 14 genera and 19 species also occur in this horizon.
Although 17 genera and 56 species are known in the Woolhope
beds, yet only 2 species are restricted to them; these are Orthis
mullochensis, Dav., and Pentamerus undatus, Sby. This last species
occurs in the Woolhope (?) of Ireland.
Every Tarannon species except Lingula Symondsw had previously
occurred, or appeared in one or other of the two Llandovery horizons
or in the Caradoc. All the species in the Denbighshire Grits except
three, Discina Morrisi, Meristella tumida, and Rhynchonella navicula,
also have appeared in and passed up from the same deposits. Thus
we find that the restricted Brachiopodal fauna (so far as we at pre-
sent know) in these beds at the base of the Wenlock is extremely
scanty.
Out of the 101 known Wenlock species, 56 had not occurred in
any earlier formation, but first appeared in the Woolhope and
Wenlock Limestone; these newly introduced Wenlock forms repre-
sent 20 genera. I deem it important to name them and give the
numbers of the species in each genus; they are :—
VNIgwAAt) Godgsosdacgac0504900000. o.species: §|) Ololtisy so peusasceses eee eeeee 3 species.
Athy Dain cccssase care sleeniands-bi- Deities Orbiculoideayeac.-ceeeree is
Orantas pecccen tee cosas ccc So One Orthig.:....Jssoshe ee eee Ons frat
(ON Acti codaudocanaddeqoqoqouandee A Re Pentamenus ys -cseee ee eeeee Sar
Diseina! tkvcerc teers coanees ge aa BRetzial since Waetenceeeeeeeeene Pap
iWichiwaldiaeeece eee ree EN 4 Rhynchonellal) -s-ceeseeee Aner,
LDS Oh AE), ma pdcagsussuscoso0coo Zieteee Siphonotretayy... cases eerie 1 ye
IGHAGWIEY, Soncssgnuebsosreooods000 oa Spirilera. 2.) wcckece eee Subs
Meristellapea tee 4 , Sirophomlenals- ceca eeeeeeee Sis ee
INucleospiraie. a--ccnsde ser gael ir foes PTriplesia..c..25. ds. saan EO Fes
Out of so large a fauna as 101 species, 96 of which occur in one
division (the Wenlock Limestone and Shale), we should expect to
ANNIVERSARY ADDRESS OF THE PRESIDENT, 16 5
find a large proportion absolutely restricted to that horizon. Of
such restricted species in the true Wenlock rocks (limestones and
shales) we have 24 or 25 per cent. None of the following species
occurs in any other horizon; and they may therefore be accepted as
definitely typical Wenlock species—<dAitrypa Barrandii, Day., Cra-
nia Grayu, Day., C. Sedquicku, Lewis, C. siluriense, Dav., Cyrtia
nasuta, Lewis, Leptena segmentum, Ang., Meristella nitida, Hall,
Nucleosptra pisun, Sow., Obolus Davidsoni, Salt., Orbiculoidea
Becketiana, Dav., Orthis equivalvis, Dav., O. basalis, Dalm., O.
Lewis, Day., O. Hughes, Dav., Retzia Salteri, Dav., Siphonotreta
anglica, Mor., Sprrifera sulcata, His., Strophomena Dayi, Dav., S.
Fletchert, Dav., S. Henderson, Dav., S. Orbignyr, Dav., S. Walin-
stedti, Linds., S. Waltont, Dav., and Triplesia MacCoyana, Dav.
The Wenlock Brachiopoda of Scotland number 11 genera and 20
species, most of them belonging to the long-range species, the more
restricted being eristella Maclaren, Hasw., Nucleospira pisum,
Sow., Orthis Lewisti, Dav., O. wenlockensis, Day., O. polygramma,
Sow., and Strophomena Henderson, Day.
The Irish Wenlocks contain 14 genera and 31 species; the most
important are Obolus Davidsoni, Salt., Pentamerus undatus, Sow.,
Lthynchonella Beltiana, Dav., R. deflexa, Sow., Orthis rustica, Sow.,
Spirifera bijugosa, M‘Coy, and Strophomena Dayi, Dav. The genera
numerically rich in species are Orthis (16 species), Rhynchonella
(10), Sperefera (8), Strophomena (16), Pentamerus (6), Meristella
(5), and Atrypa (5). The rarer genera are but feebly represented.
12 genera and 32 species pass to the Lower Ludlow, 10 genera and
20 species appear in the Aymestry, and 11 genera and 17 species in
the Upper Ludlow. Again, the Wenlock is allied to the Caradoc
and Llandovery groups through 11 genera and 41 species, 59 being
Upper Llandovery, 22 Lower Llandovery, and 14 Caradoc species ;
5 Llandeilo species lived on through all five periods, viz. Lepiena
sericea, Orthis biforata, O. calligramma, O. elegantula, and Stropho-
mena rhomboidalis.
LAMELLIBRANCHIATA.—Out of the 16 genera and 44 species of
bivalve shells ranging through the Wenlock rocks, the upper divi-
sion or Wenlock Limestone yields 43 species, the one absent or
uncertain form being doubtfully Lunulacardium aliforme, Sby.
The Tarannon Shale contains, so far as we know, only 2 species,
and both are Upper Llandovery shells, Pierinwa planulata, Conrad,
and P. retrofleca, Wahl.; both pass to the Ludlow beds. The Den-
bighshire Grits from all available sources yield 7 genera and 10
species. The Woolhope only 3 genera and 5 species: these, with
the Denbighshire-grit species, are all Upper Wenlock also. The
local stratigraphical position of the ‘“* Woolhope or Barr” Limestone
carries with it occasionally a peculiar fauna, and, although strictly
of Wenlock age, there is always uncertainty as to the occurrence of
few or many species, but it is next in numerical value to the Upper
Wenlock. The Wenlock rocks of North Wales furnish 8 genera
and 14 species, Pternea, Cardiola, and Cucullella being the chief
genera. Pterinea has yielded 6 species, Cardiola 3, and Cucullella
VOL. XXXVI. n
166 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
3: other genera (Avicula, Arca, &c.) only one or two species
each.
In South Wales 11 genera and 26 species have been collected.
The genera are the same, but with specific additions to Modiolopsis
and Mytilus.
Of the 3 Irish genera the 6 species are—Pterinea lineata,
Goldf., P. planulata, Conr., and P. retrofleza, Wahl., Cardiola
Jibrosa, Sow., and C. interrupta, Brod., with Goniophora cymbeformis,
Sow.; none are confined to the Irish beds. Only 5 genera and 8
species of Lamellibranchiata are really peculiar to the Wenlock
series. 7 genera and 15 species came in from the Upper Llandovery;
3 of these 15 are Lower Llandovery also, viz. Pterinea retroflexa,
Cardiola interrupta, and Mytilus mytilimeris; 2 of the same are
Caradoc, and 3 species came direct from the Caradoc; they are
Pterinea tenuistriata, M‘Coy, Arca (Palearca) edmondiuformis,
M‘Coy, and Ctenodonta anglica, D’Orb. Thus the Wenlock is united
to the Upper Llandovery below through 17 species, and to the Lower
Ludlow above by 21 species, and these all pass to the Upper Ludlow,
so that the actual number of peculiar Lamellibranchs, or the
Bivalve fauna, is reduced to the following 8 species :—Ambonychia
tumida, Sollas, Pterinea asperula, M‘Coy, and P. laminosa, Goldf.,
Cleidophorus planulatus, Conr., Modiolopsis acutipora, Sollas, M.
inflata, var., and M. chemungensis?, Conr., with Mytilus ungweu-
latus, Salt. Nevertheless, assuming that the transgressional species
also strictly belong to the rocks in which they occur, the Wenlock
Bivalve fauna consists of 25 species by retaining those forms that
pass up to the Ludlow.
GastERoPoDA.—Looking at the splendid Ccelenterate, Echino-
dermal, Crustacean, and Brachiopodal faunas in the Wenlock series,
the distribution and ranges of which we have analyzed and tabu-
lated, we should have expected this class to have been more
largely represented, especially as during the- Caradoc and Upper
Llandovery periods a larger molluscan fauna existed, although
apparently the nature of the sea-bed was not so favourable as that
of the more calcareous and argillaceous condition of the Upper
Wenlock, in which the great mass of the Wenlock fauna occurs.
All the genera belong to the order Prosobranchiata and division
Holostomata. The Caradoc Gasteropoda, as we have seen, number
14 genera and 53 species, the Wenlock 9 genera and 27 species ;
the 9 genera represent 5 families. One species only occurs in the
Tarannon Shale (Acrocula haliotis), and ranges through to the
Wenlock Limestone and Ludlow. The Denbighshire Grits contain
Acroculia haliotis, Holopella gracilior, Loxonema elegans, Murcha-
sonia articulata, and M. Lloydi, or 4 genera and 5 species. ‘The
Woolhope exhibits but a small fauna, only 8 species, 4 of which are
Euomphali and 2 Acroculie, with Trochus (Cyclonema) exaltatus and
Turbo tritorquatus. In this, as in all the other classes, nearly every
species known occurs in the Upper Wenlock; thus the 9 known
genera and 24 out of the 27 species belong to that horizon. 7 genera
and 17 species occur in South Wales, but only 1 in Scotland
ANNIVERSARY ADDRESS OF THE PRESIDENT. 167
(Euomphalus furcatus). Ireland yields 4 genera and 5 species
(Murchisonia articulata, M. Lloydii, Euomphalus alatus, Cyclonema
corallii, and Acroculia haliotis). We must remember that 5 genera
and 6 species range from the Upper Llandovery; these are Huom-
phalus alatus, Sow., HE. furcatus, Sow., E. sculptus, Sow., Holopella
obsoleta, Loxonema sinuosa, Sow., and Murchisonia articulata, Sow., 2
of the same occurring in the Caradoc, namely—Luomphalus alatus,
Sow., 2. sculptus, Sow., and probably Turbo tritorquatus, M‘Coy ; and
5 of these same 6 range to the Ludlow. Only 17 species out of the
27 strictly belong to the Wenlock rocks proper. At present we
know of no species other than those in the division Holostomata
in the Silurian rocks. Hunema is the only new genus that appeared
in this formation; £. cirrhosum is a South-Wales species.
Preropops.—Only 3 species, Conularia Sowerbyu, Defr., Theca
anceps, Salt., and J. Forbesii, Sharpe, have as yet appeared in the
Wenlock group; none of the 3 occurs in the Tarannon Shale, in the
W oolhope beds, or in Ireland. Theca Forbesii has been found in
the Denbighshire Grits and Wenlock Limestone, and passes upwards
to the Upper Ludlow. JZ. anceps is here Wenlock only, but is a Cara-
doc species also. Conuwlaria Sowerby: first appeared in the Caradoc,
and, with the exception of the Upper Llandovery, is present in all
‘horizons up to the top of the Upper Ludlow; it also occurs in the
Scotch beds. The only form of Thecosomatous Pteropod that trans-
gresses the Silurian rocks is Conularia, which is Devonian and
Carboniferous; but in Britain Conularia has not occurred in the
Devonian series, although its associate, Bellerophon, is represented by
5 British Devonian forms, 2 occurring in the Lower, 1 in the
Middle, and 4 in the Upper Devonian. Conularia Sowerby: and
Theca Forbesiz both pass to the Upper Ludlow.
Hereropopa.—This pelagic order is well represented in the Wen-
lock beds through Eecculiomphalus levis and 7 species of Bellerophon ;
but no species is confined to or specifically characteristic of the
Wenlock beds. All had previously occurred either in the Caradoc
or Llandovery rocks. Hcculiomphalus levis, Bellerophon trilobatus,
and B. carinatus range into the Upper Ludlow beds ; none occurs in
the Tarannon Shale; 3 species are known in the Denbighshire Grits
(Bellerophon trilobatus, B. expansus, and B. carinatus), and 3 in the
Woolhope beds (B. bilobatus, B. dilatatus, and B. trilobatus). In
the Wenlock Limestone we know of 4 species of Bellerophon and
Ecculiomphalus levis. B. dilatatus is the only form known in
Ireland; and Scotland yields none. The 3 species passing up or
ranging into the Ludlow series are Ecculiomphalus levis, Bellerophon
trilobatus, and B. subdecussatus ; there are none in the Aymestry
Limestone.
CEPHALOPODA.—5 genera and 30 species of the order Tetra-
branchiata, illustrating the Nautilide and Orthoceratide, are known
in the Wenlock rocks: all but 3species are represented in the Wen-
lock Limestone and Shale ; these 3 are Woolhope species ( Actinoceras
baccatum, H. Woodw., Lituites cornu-arietis, Sow., and Orthoceras coni-
cum, Sow.). Actinoceras baccatum is essentially a Woolhspe species,
R2
168 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
described by Dr. H. Woodward, and the only one known from the
Woolhope beds of Little Hope. Lituctes cornu-arietis, Sow., and
Orthoceras conicum, Sow., although not ranging higher than the
Woolhope beds, appeared in the Llandovery, and help to connect
the Lower Wenlock with the Upper and Lower Llandovery. In
the Denbighshire Grits we have almost unexpectedly 3 genera and
7 species, only 2 of which are of Llandovery age (Orthoceras tenui-
cmctum, Portl., and @. subgregarwum, M‘Coy). The remaining 5
species pass from the Denbighshire rocks, where they are first known,
to the Upper Wenlock ; they are O. primeevum, Forbes, O. tracheale,
Sow., O. ventricosum, Phragmoceras nautilewm, and Cyrtoceras ibea.
26 of the 30 species occur in the Wenlock Limestone and Shale; 13
range through South Wales, and 12 through North Wales, 7 belonging
equally to North and South Wales. The only 3 Irish species known
are Orthoceras (Creseis) primevum, Forbes, O. subundulatum, Portl.,
and O. tenuiconctum, Portl.; and the 3 Scotch forms are O. Maclareni,
Salt., O. subundulatum, Portl., and O. tenwemctum, Portl. 11 species
pass to the Lower Ludlow; 2 of these, and the only 2 known
(latuites giganteus, Sow., and Orthoceras angulatum, Wahl.), pass
to the Aymestry Limestone; and 3 genera and 8 species range to the
Upper Ludlow; thus only 4 genera and 9 species out of the 30
are really Llandovery, or these 9 species come up from the Llan-
dovery and Caradoc.
The accompanying Table shows the numerical history of the 14
classes. The first four columns illustrate the stratigraphical distri-
bution of the species through the Tarannon beds, Denbighshire
Grits, Woolhope beds, Wenlock Shales and Limestone, indeed all the
formations above the Upper Llandovery. The succeeding five
columns show the geographical distribution of the species through
North Wales, South Wales, Westmoreland, Scotland, and Ireland ;
and to show still further the connexion between the Wenlock and
Ludlow fauna, I have stated in the remaining or last three columns
the number of species that pass to the three divisions of the Ludlow
group, in which it will be seen that out of the 171 genera and 536
Wenlock species, 71 genera and 126 species pass to the Lower
Ludlow, 38 genera and 52 species to the Aymestry, and 51 genera
and 87 species to the Upper Ludlow; any higher transgression from
the Ludlow into the Devonian is given under the Ludlow table.
There are only 20 species, including the 6 Fishes from the passage-
beds and the 8 species of Merostomata, that range through the
Ludlow series. The oldest fish-remains occur in the Lower Ludlow,
Scaphaspis ludensis, Salt., being the oldest species known.
169
ANNIVERSARY ADDRESS OF THE PRESIDENT.
| From Upper Llandovery.
Plante.
Classes.
JEARO UB OVAOIEN © So ndedeAeaonanabaneses ea.
Hydrozoa ...... Secuene
ACtInIOZ02 \...¢.--. ate a CAGE
HKehinodermata..... Arata Teohea
Annelida
Crustacea ........... SI or eee ate
beoseersvesarsess ree eercsees
Bryozoa
IB GAC AIO DOC ames me ease
Lamellibranchiata ..
2200S ea eser
Gasteropoda......... Pesea ean Cnataa
Picropodae cae.
etOLO MOM Gir cacenmtacanetasneacm aes
Caphbalopodas, «.csj<avscs.eastacrse
Coes eoeeeeessoseae
Taste XITI.— Wenlock.
Stratigraphical Geographical
Distribution. Distribution,
a
at
"5
re O cS cn ; . rd
rb) 2 2 rm f wo nD S|
“2 oe} De eee |e
=| a 3, aoe nee ee ©
Sas Se) ee Piss ton Ge
S i= — —s Ff = ts S
S| Se) ese] Swe ps
rH q fe) @). |} > bs S ) Oo
eS o = [es a) i) iS 5
HA Fi4liale ia
2 1 3 1 1 1
2 1 3 1 1 1
5) 1 3 3 3
23 : r 0 8 15 16 5
2 2 16 25 7 10 8
5 3 26 76 11 1&8 sxe 11
1 2 28 1 4
* 1 2 65 1 5 00
1 3 13 4 4
sf 1 3 34 4 6 ©
6 3 14 2.7 5 9 s
8 5 2:5 74 11 14 3
3 10 2
4 24 eee 2 e
10 14 17 21 9 12 11
15 19 06 96 23 39 20
1 7 3 15 8 11 ?
2 10 5 43 14 26
1 4 4 9 E 7 1
1 5 8 24 8 al te " 1
l 3 1 1 1
ee 1 ee 3 1 i « 1
1 1 2 1 1
Mins 3 3 5 4 3 9
3 3 5 4 3 1
vi 4 26 12 13 3
26 39 67 1G1l R47 68 3 29
54 57 137 473 98 160 16 45
* In the column headed Wenlock beds I omit the Rhabdophora; they appear in the localities,
Pass to
Lower Aymestry Upper
Ludlow. Limestone. Ludlow.
3 2 2
3 2 2
1
2
9 ee 4
16 8 7
4 1 2
6 1 2
3 3 4
4 3 6
13 5 8
18 6 10
2 1
2 1
12 10 iil
32 20 17
13 3 9
21 3 24
6 4 4
9 6 6
2
Be Uh 2
2 2
Pee ne {he tens. 2
TPs 2 3
11 2 3
71 38 51
126 562 817
170 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Luptow.
392 species, representing 137 genera, is, as nearly as can be ascer-
tained, the numerical value of the Ludlow fauna. No true Ludlow
rocks are certainly known to occur in North Wales, excepting
perhaps in a small part of Montgomeryshire, south-east of Newtown.
The Ludlow formation is zoologically allied to the Wenlock through
129 species. The chief classes, or those most represented numeri-
cally, are the Actinozoa with 12 genera and 17 species, the Echino-
dermata with 12 genera and 21 species, the Crustacea with 29 genera
and 97 species, the Brachiopoda with 13 genera and 48 species, the
Lamellibranchiata with 17 genera and 71 species, the Gasteropoda
with 9 genera and 33 species, the Cephalopoda 6 genera and 37 species,
and lastly the Vertebrata, which first appear through the Fishes,
represented by 10 genera and 14 species, omitting the genus Onchus,
the remains of which may be “telsons” or tail-spines of Crus-
tacea. The comparatively small fauna of the Aymestry Lime-
stone (53 genera and 84 species) is, although local, a remarkable
one, and clearly shows the nature of the sea-bed and sedimentary
material in relation to the habits of life of the species represented.
Mostly it is a recurrent fauna from the Wenloek, 57 species being
common to the two, these 57 representing 38 genera, clearly showing
the rarity and paucity of species illustrating the genera, and the
lenticular or accidental nature of the Aymestry Limestone between
the Lower and Upper Ludlow beds. The classes that appear to be
most fully represented are the Coelenterata (Actinozoa), the Crusta-
cea, Brachicpoda, Gasteropoda, and Cephalopoda. No fish-remains
are known, although the two Ludlow series contain them*. The
feeble representation of the Ludlow rocks in North Wales, as before
stated (only 19 species), by comparison with Westmoreland (127)
calls for critical examination into the physical rather than the pale-
ontological aspect of the question; and this is still more prominently
seen through the still larger fauna in South Wales and Shropshire,
the former yielding 163 species, the latter 187; and further through
the intermediate areas termed Herefordshire (where 114 species are
known) and Worcestershire (121). Could we but see and examine
the continuity of the old Wenlock and Ludlow sea-bed and its
deposits between Denbighshire, Westmoreland, and the south of
Scotland, now under the St.-George’s Channel (or denuded away),
we should doubtless find traces of the Lower Wenlock and Ludlow
rocks, uniting the two now disunited areas. We cannot doubt that
this continuity once existed, though probably the rocks of the two
areas were deposited under very different and local conditions.
Petrologically they essentially differ ; but paleeontologically or speci-
fically in certain groups the agreement is close and decisive, omit-
ting the largely represented Annulose or Crustacean orders Meros-
* Mr. Salter included the Aymestry Limestone with the Lower Ludlow, as
being a calcareous condition of it. Mr. Lightbody was always impressed with
the fact that the calcareous nature of the beds above the Aymestry Binatone
influenced the fossils to a marked degree.
ANNIVERSARY ADDRESS OF THE PRESIDENT. I71I
tomata and Phyllopoda in the Ludlow rocks (45 species), which
stand alone as a peculiar and local group; their presence there-
fore need not enter into the calculation*. The great extension of
the Wenlock promontory to Wellington, running parallel to the
Dudley beds, and the overlap and cover of the Triassic rocks to the
north on to the Mersey, Liverpool Bay, Lancaster and Morecambe
Bays, go far to lead us to believe that the missing evidence of
the agreement between the Ludlow of the two areas of Wales and
Westmoreland, as well as the unsatisfactory correlation of the Den-
bighshire Grits and Tarannon Shales with the rocks of the Lake
country, can be accounted for ; for it must be admitted that much has
yet to be done with these Lower Wenlock rocks of Denbighshire,
Westmoreland, &c. The Kendal group (or the Ludlow rocks) and
the Ireleth Slates, which are the equivalents of the Wenlock of the
south, can certainly be correlated paleontologically, dissimilar as they
appear physically. The Scotch uppermost Silurians are exhibited
only in three localities; to the south of Kirkcudbright and in the
Pentland Hills both the Wenlock and Ludlow groups occur. The
American series termed the Lower Helderberg group are the true
equivalents of our Lower and Upper Ludlow, and contain a number
of species in common. ‘The exact equivalent of the Oriskany Sand-
stones may be our lowest Devonian. In North America their place
is either at the top of the Upper Ludlow or between that and the
lowest Devonian rocks, or ‘‘Corniferous beds” of the American
geologists. I now attempt to analyze the extensive fauna of the
Ludlow group, accepting the triple division unconditionally ; or, in
other words, retaining the Aymestry Limestone as a distinct subfor-
mation, not attached either to the Lower or the Upper Ludlow; its
accidental position carries with it certain fossils having an important
bearing upon physical geology.
Prantra.—For the first time above the Wenlock we meet with what
may be termed plants proper; yet the two genera Chondrites and
Fucowdes are doubtful. 5 genera and 5 species are known; 4
species occur in the Upper Ludlow, and 3 of the same in the
passage-beds between the Upper Ludlow and Lower Old Red Sand-
stone ; none are known in the Lower Ludlow or the Aymestry beds ;
nowhere in the Ludlow of either South or North Wales, Westmore-
Jand, or Ireland are plant-remains known. Actinophyllum plicatum
occurs in Shropshire and Herefordshire; Chondrites verisiemilis 1s an
Upper Ludlow form in Scotland. The seed-like bodies of doubtful
affinities (Pachytheca spherica) occur in the tilestones and bone-bed
of the uppermost Ludlow of Shropshire, Worcestershire, and Here-
fordshire. Actinophyllum and Pachytheca here first occur, and do
not pass to the higher formations. The passage-beds contain Acti-
nophyllum plicatum, Chondrites verisimilis, Pachytheca spherica,
and Pachysporangiwm pilula. 15 species of Crustacea, 19 species
of Lamellibranchiata, 6 species of Gasteropoda, 4 species of Hetero-
poda, and 6 species of Fish, or nearly 70 species, illustrate 10 classes
* Phyllopoda (Ceratiocaris 14 species), Merostomata (Hurypterus 10 species,
Hemiaspis 6, Pterygotus 9, Slimonia 3, and Stylonurus 3).
172 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
in this borderland between the Upper Ludlow and the Old Red
Sandstone.
Prorozoa.—A series of sponges (Calcispongie) numbering 7 genera
and 10 species occur in the Ludlow rocks, 3 of which are also
Wenlock. 6 genera and 8 of the species belong to the Upper
Ludlow; Amphispongia, Favospongia, and Tetragonis are new
forms, and appear for the first time, and, with Mavospongia Ruthven,
Ischadites Kenigr, and 4 species of Spongariwm, die out in the
Upper Ludlow. 3 genera and 5 of the species occur in the Ludlow
beds of Westmoreland; they are Favospongia Ruthven, Spongarium
equstriatum, S.imterlineatum, S. interruptum, and Tetragonis Danbyt.
The conformable Old Red Sandstone in the Ludlow area, or anywhere
along the extended strike and junction of the two formations, con-
tains nothing in common with the Upper Ludlow save a few fish
and crustacean remains, all ceasing with the Downton beds and
tilestones. The Eurypterids (Sty Wlowan us megalops and Hurypterus
pygmeus) pass to the lower beds of the Old Red Sandstone; but
through all the Old Red of South Wales (or the Silurian area) or
Gloucestershire or Somersetshire, from its base to its junction with
the Lower Carboniferous, nothing has occurred save fragments of
Cephalaspis and Holoptychius, no other class in the animal kingdom
being represented.
Hyprozoa.—Only 1 genus and 8 species of this class seem left to
bring to a close the history of the Graptolite group of the Hydrozoa.
Monograptus has 8 species, which are all Lower Ludlow and occur
in the Ludlow area. In no region of the globe where the Silurian
rocks have been deposited have any species of this class trans-
eressed or passed into higher formations. About 210 species belong-
ing to 30 genera have lived during the Silurian epoch, ranging from
the Arenig with 42 species, the Llandeilo 44, Caradoc 38, Lower
Llandovery 50, Upper Llandovery 12, Wenlock 23, to the Ludlow
with 8, their maximum development being at the commencement
of the Lower Silurian of certain systematists. They came into
existence with unexampled prodigality and suddenness, but gradu-
ally died out as conditions grew less and less favourable for their
sustenance and development. America, Bohemia, Scandinavia,
Australia, and Britain have all largely possessed the same hydrozoal
fauna, illustrating the same or similar deposits. Whether homo-
taxially or not, most of the same genera have occurred in rocks
of the same age as those of the british Islands, and always under
the same physical conditions. The labours and researches of Hall,
Barrande, Geinitz, Linnarsson, Nicholson, Lapworth, Hopkinson,
Carruthers, and M‘Coy in this field of zoological history will ever
reflect honour on their memory. To Mr. Lapworth graptologists
owe much; no other author has given such attention to the Rhab-
dophora, whether we regard his specific work or that devoted to
their history and geological distribution through time, and his phi-
losophical views relative to their affinities, structure, and systematic
classification.
Actinozoa.—Not a single species out of the 17 occurring in the
ANNIVERSARY ADDRESS OF THE PRESIDENT. DRS
Ludlow beds strictly belongs to them or is confined to the Ludlow ;
all have previously occurred in the Wenlock. 17 species are Lower
Ludlow; 8 of the same occur in the Aymestry Limestone, and
7 in the Upper Ludlow, chiefiy the Favosites (5 species) ; 13 species
occur in Shropshire, 6 in Westmoreland, and 12 in Worcestershire.
Monticulipora papillata is the only Scotch species known. 6 species
occur in Ireland (Fwosites asper, F. cristatus, F. fibrosus, Alveolites
Labechu, Cr yathophyllum truncatum, and Monticulipora papillata)
only 1 species is known in North Wales (Heliolites tubwlatus) ; and.
6 genera and 9 species in South Wales. ‘The accompanying Table,
showing their geographical distribution, will be clearer than descrip-
tion, where the species are so irregularly distributed.
oO .
3 eeliccs
Ri es see ob ve
o © e oS “3 3S
Cet] Se a il
O + S 5
Ludlow Species. Peal ete Hee eral Et resem ee
le eaten = | ts
ete ara SS ath By eles
as) = (e) S © on) Gs | &
S B = S a On| Wasa eees
S) Sees) is = So | =
aD |) 24 |p| Eo es ca |
Alveolites Labechii .................. % % % % *
Coomites mbertextus .c.2..<.5 .csecss. *
Cyathaxonia siluriensis ............ ea al wae
Cyathophyllum truncatum ......... “3 % ae *
Favosites GDSTTE “yscqssoandodnosdaroce % % * Benalla %
cristatus SE TaN ota eae baa. || sc00 * ae * x
Bee =A DNOSUG CS AS ticle osu -wetdc dev doek % x * % %
—— gothlandicus ....... pactasaets * x | * | x
Horbesi.
Fistulipora decipiens.
Halysites catenularius............... See ae le %
Heliolites interstinctus ............ Sean |e 0) |e ¥ % x
fubulatus.....s..:. EC or ne AOA ae asst * * %
Monticulipora papillata ...........- Stay eeu kere Ana Deen fe IE gh 9G- hea
Ompbyma turbinata ..............- Ree ee Sea aes | aE *
Pabraley OYA. ......+csceey ese Repth arr Ser diese malts | Fae
Syringopora bifureata.......... oobl|.cok: |leodoin lesion lle we
Be MPCUISE waht vssiaeshiewies sacievee * % *
9 US Aa 76 6 1 6
EcurnopERMATA.—This group in the Ludlow comprises 12 genera
and 21 species. There are 3 genera and 4 species of Crinoidea
(Actinocrinus pulcher, Ichthyocrinus pyriformis, I. M‘Coyanus, and
Taxocrinus @Orbignyt). Of the remaining 17 species 4 are Cys-
tideans (Hchinocystites pomum, H. uva, Pseudocrinites maguificus,
and P. quadrifasaatus), all Lower Ludlow; and 13 Asteroidea.
2 species of Palwaster (P. Ruthvent and P. hirudo) and Pale-
asterina primeva, with Protaster Sedgwicku, occur in the Upper
Ludlow of Kendal, Westmoreland. 4 Palwocome (P. Colvini, P.
cygnipes, P. Marston, P. vermiformis) are all Lower Ludlow from
the Leintwardine beds near Ludlow. Palwodiscus ferox, Protaster
leptosoma, P. Miltom, and P. Sedgwicku are from the same horizon
and locality, as well as Rhophalocoma pyrotechiica—Shropshire thus
174 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
yielding 8 species of Lower Ludlow starfishes and Westmoreland
4 Upper Ludlow. The Lower Ludlow Echinodermata therefore
number 11 genera and 19 species, the Upper Ludlow 6 genera and
7 species. None occur in Herefordshire, Scotland, or Ireland. 4
genera and 7 species (3 Crinoidea, 1 Cystidean, and 3 Asteroidea)
came from the Wenlock beds. In the Ludlow promontory and all
along the line that marks the junction of the Old Red Sandstone
with the Upper Ludlow all Silurian life ceased. The slow elevation
of that region caused the Silurian Annuloid fauna to dwindle and
pass away almost entirely. No vestige of it again appeared in the
true Old Red area anywhere; and the want of evidence to show
what rocks may be below the Lower Devonian of the Devonshire
and Somersetshire areas leaves the question of stratigraphical or
zoological continuity one of doubt and in the region of the unknown.
Ireland or North Devon may yet solve the problem, for it is here
we should expect it. The new Ludlow genera were Hchinocystites,
Paleasterina, and Tetragonis, none of which leaves any successors
behind, none being known either in the Devonian or Carboniferous
rocks.
ANNELIDA.—The Annelida are a singular group in the Ludlow
rocks; 9 genera and 17 species have been obtained from the several
horizons (4), and their geographical distribution is wide also. 15
species occur in the Upper Ludlow; the characteristic Cornulites
serpularvus is the most abundant, occurring at all 4 horizons, and
in all localities except Shropshire and Ireland. The Lower Ludlow
has yielded Cornulites serpularius, Serpulites dispar, S. longissimus,
Spirorbis Lewisv, and Trachyderma squamosa. The Aymestry Lime-
stone contains 4 species, all of which are also in the Lower Ludlow.
4 of the 17 species are also Wenlock. 3 species of Afnonites and
3 species of Arabellites, belonging to the order Polycheta, are
determined from jaw-remains by Mr. G. J. Hinde*; they are Upper
Ludlow, and help to swell the Annelide fauna. 3 species of the
order Tubicola occur in the Passage-beds. 9 species range through
South Wales, North Wales has 4, Westmoreland 6, Shropshire 5,
Worcestershire 7, Herefordshire 4, and Scotland 3; but none, so far
as I can ascertain, occur in Ireland.
Crustacra.—The two great orders of the class Crustacea in the
Ludlow rocks are the Merostomata and the Phyllopoda. Of the
former we know 32 species—Lurypterus 10, Pterygotus 9, Himan-
topterus 1, Slimona 3, Stylonurus 3, and Hemiaspis 6. Of the
latter, through Ceratiocaris and Dictyocaris, we have 16 species ; and
there are possibly one Amphipod (Necrogammarus Salweyr) and a
Peecilopod (Neolimulus falcatus, Woodw.). These 32 species of
Merostomata and Peecilopoda swell up the Crustacean fauna at the
expense of the Trilobita, which number only 10 genera and 20
species, 2 genera only of the 10 (Homalonotus and Phacops) passing
to or occurring in the Devonian rocks. The Ostracoda number
5 genera and only 13 species. The Crustacean remains termed Asta-
coderma by Dr. Harley, number 14 so-called species; all are in the
* Quart. Journ. Geol. Soc. vol. xxxvi. pp. 368-376.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 175
Lower Ludlow. The whole Crustacean fauna, therefore, of the
Ludlow rocks is 29 genera and 97 species. The Lower Ludlow
contains 18 genera and 47 species, the Aymestry Limestone 9 genera.
and 12 species, and the Upper Ludlow 23 genera and 71 species.
The Passage-beds into the Old Red Sandstone have yielded 9 genera
and 15 species, 4 being Ostracoda, 1 Phyllopod (Ceratiocaris decorus),
and 10 Merostomata (Eurypteride). No Trilobite occurs in the
Passage-beds. This Passage-bed Crustacean fauna is what we
should have anticipated ; the Brachiopoda and Mollusca proper show
the same indications of a change from a deeper to a shallow coast-
line, and a fauna struggling to maintain life against new and adverse
conditions. Shropshire through the Ludlow area possesses 18 genera
and 46 species, Worcestershire 17 genera and 25 species, Hereford-
shire 14 genera and 26 species, Westmoreland 8 genera and 15
species. Scotland, chiefly through the Phyllopoda and Merosto-
mata, has 12 genera and 22 species. Ireland only possesses 2
(Calymene Blumenbachu and Phacops caudatus). This deficiency of
the Crustacea in Ireland, as indeed of all the classes except the
Brachiopoda, bears out the fact of the smallness of the Ludlow
fauna in Ireland. I am obliged to carefully detail the number of
genera and species that range through and enter into the distri-
bution of the Crustacean fauna on account of its peculiarities.
13 new genera made their appearance during the Ludlow period.
4 Ostracoda, Cypridina, Entonus, Kirkbya, and Moorea ; 4 Merosto-
mata (Hurypterida), Himantopterus, Slimona, Stylonurus, and
Parka; Xiphosura 1, Neolumulus; Phyllopoda 1, Dictyocaris ; Am-
phipoda 1 ?, Necrogammarus ; Crustacean remains, Astacoderma (14
species). 3 genera (Stylonurus, Cypridina, and Parka) occur in
the Old Red Sandstone, but not in connected areas. 16 genera and
26 species are common to the Wenlock and whole of the Ludlow, thus
reducing the true Ludlow Crustacean fauna to 71 species instead of 97.
Bryozoa.—Heteropora crassa, Cerropora sulcata, and Ptilodictya
lanceolata are the only 3 Ludlow Bryozoa. The first and last are
Wenlock also. They occur in the Lower Ludlow and Aymestry
Timestone of Worcestershire and Shropshire. Ceriopora sulcata
occurs in the Ludlow of Ireland. No species occurs in the Upper
Ludlow or Passage-beds, either in South or North Wales, West-
moreland, or Scotland. The nature of the Ludlow shales and mud-
stones doubtless was the cause why the Actinozoa, Hydrozoa, Kchi-
nodermata (Crinoidea &c.), and Bryozoa, all mostly dwellers in clear
water, are so sparingly developed and distributed through the Ludlow
rocks, the Aymestry Limestone being of little palaeontological value
owing to its lenticular disposition, mode of occurrence, and uncertain
continuity.
Bracuropopa.—Although by no means a small fauna, the Ludlow
Brachiopoda numbering only 48 species and 13 genera are less
than half as numerous as those of the underlying Wenlock rocks.
41 of these 48 had hved in the Wenlock seas and passed to the
Ludlow ; therefore only 7 species are Ludlow proper; and only 3
species passed to the Devonian—Altrypa reticularis, Strophomena
176 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
rhombordalis, and Lingula cornea. The last named in the Ludlow
country passes into the lowest beds of the Old Red Sandstone. The
others named are “ Devonian” of the North and South Devonshire
areas, and not known in the Old Red proper. In the Passage-beds
into the Old Red of Herefordshire, Shropshire, and Worcestershire
some 5 or 6 species occur; they are Chonetes striatellus (latus), Dis-
cma rugata, Lingula cornea, Lingula nanima, and Strophomena
rhomboidalis. They are associated in places with a few Asiphonida
of shallow-water habits, Pterinea, Modiolopsis, Orthonota, &e. ‘The
Lower Ludlow has yielded 13 genera and 38 species, 33 of which
are Wenlock. 12 genera and 25 species occur in the Aymestry
Limestone, and 11 genera and 24 svecies in the Upper Ludlow; but
no genus is peculiar to either the Aymestry or Upper Ludlow beds,
the whole being represented in the Lower zone.
‘The only species in the Ludlow not Wenlock are Lingula cornea,
L, lata, Orthis canahculata, O. lunata, Rhynchonella pentlandica, and
Strephomena ornatella. In other words, only these 6 species of
Brachiopoda are really Ludlow forms. No species is known in
North Wales, but 28 have been collected in South Wales. Here-
fordshire, Worcestershire, Shropshire, and Scotland have each yielded
11 genera, and respectively 23, 27, 30, and 15 species; Westmore-
land has 8 genera and 14 species ; Ireland 9 genera and 18 species.
LAMELLIBRANCHIATA.—Both the Lower and Upper Ludlow pos-
sess a large Molluscan fauna; the Lower 14 genera and 54 species,
and the Upper 15 genera and 56 species; the intermediate Ay-
mestry Limestone only 4 genera and 7 species—Pterinea lwans,
P. retrofleca, P. Sowerbyi, Cardiola striata, Grammysia cingulata,
Orthonota rotundata, and O. semisulcata. The chief genera are Pte-
rincea with 12 species, Anodontopsis 7, Orthonota 16, Modiolopsis 5,
Ctenodonta 4, Cucullea 4, and Grammysia 4 species. The Passage-
beds contain 9 genera and 19 species, yet no single species occurs in
the Lower Old Red Sandstone; with the change of lithological
characters all life seems to cease also, or no record is left. For the
life-history of those rocks, equivalent in time to those of the Old Red
Sandstone in the classical Silurian area, we have to consult the De-
vonian series of North and South Devon and Cornwall, where a
fauna unsurpassed in perfection, if not in magnitude, in all the in-
vertebrate classes exists—a group made famous in British geological
history through the labours and researches of Sedgwick, Murchison,
De La Beche, and Phillips. Westmoreland and Cumberland, through
the researches of Sedgwick and M‘Coy, Harkness and Nicholson, in
the Kendal area, exhibit a large Ludlow Lamellibranchiate fauna ;
12 genera and 37 species are known. Shropshire has 9 genera and
16 species, Worcestershire 8 genera and 17 species, Herefordshire 6
genera and 12 species, Scotland 6 genera and 13 species, and Ireland
only 2 genera and 3 species. North Wales hitherto has yielded only
1 genus and 4 species; 13 genera and 21 species ranged from the
Wenlock into the Ludlow, thus altering the numerical value of the
Ludlow bivalves proper to 50 species, none of which passed the
Passage-beds between the Upper Ludlow and Old Red Sandstone.
ANNIVERSARY ADDRESS OF THE PRESIDENT. Maa
Extensive patches of Upper Silurian rocks on the eastern side of the
Silurian area and border of the Old Red, such as Woolhope, Usk,
the long strike of the Malverns on to May Hill, thence across the
Severn at Purton Passage to Tortworth, indicate great physical
changes in the borderland between the fossiliferous Upper Silurian
and the unfossiliferous Old Red; and whatever change brought in
the marine Devonian of North Devon, south of the Mendip axis and
on the same strike, and all the South-Wales Old Red beneath the
South-Wales coal-field to the Bristol Channel, certainly must ac-
count for the loss of all the Ludlow species ; that the Devonian area
was one of long and continuous depression south of the latitude of
the Mendips there cannot be any doubt, and probably the mass of
Old Red Sandstone occupying Caermarthenshire, Monmouthshire,
Breconshire, Herefordshire, and Worcestershire was being at the
same time slowly elevated.
GasTEROPODA.—9 genera (six of which had appeared in the
Wenlock) and 33 species, 11 of which were also Wenlock, range
through the Ludlow rocks; the Lower Ludlow has yielded 8 genera
and 15 species, the Aymestry Limestone 5 genera and 11 species,
and the Upper Ludlow 9 genera and 21 species. 3 genera and
6 species occur in the Passage-beds into the Old Red Sandstone ;
they are Holopella conica, H. gregaria, Holopea obsoleta, Mur-
chisonia torquata, Platyschisma helicites, and P. Williamsi. They,
however, cease here, none living into the red beds of the Old Red
Sandstone. North Wales has yielded only 2 species, Holopella
gracilior and H. gregaria ; Scotland only 4 species, Acroculia anti-
quata, Huomphalus funatus, Platyschisma semulans, and P. helicites ;
Ireland has only registered 1 species, Huomphalus alatus; Here-
fordshire 7 genera and 11 species, Worcestershire 6 genera and 9
species, Shropshire 7 genera and 14 species, and Westmoreland 6
genera and 14 species. 6 genera and 13 of the 33 species come up
from the Wenlock and range through the Ludlow rocks; they are
Acroculia haliotis, Cyclonema coralli, C. octavia, Kuomphalus alatus,
E. carinatus, E. funatus, H. rugosus, Holopella gracilior, H. obsoleta,
Loxonema elegans, L. sinuosa, Murchisonia Lloydi, and Mu. ar Beclaties.
9 species only are Lower Ludlow. All become extinct in the Tile-
stones and Passage-beds.
Preroropa.—Conularia subtilis and C. Sowerbyi, with Theca
Forbesi, are all the species (3) illustrating this pelagic group. ‘The
two last named are Upper Ludlow. Neither the Aymestry Lime-
stone, Passage-beds, North Wales, or Worcestershire yield either
species, nor ‘do we know of any species in Ireland. C. Sowerbya
occurs in Scotland; all 3 species in Westmoreland and 2 (Theca
Forbes and Conularia Sowerby yt) in Shropshire. These last are also
Wenlock species.
Hereroropa.— Bellerophon (6 species) and Heculiomphalus levis
constitute the Ludlow stock of Heteropoda. Heculiomphalus levis,
Bellerophon expansus and B. dilatatus occur both in the Lower and
Upper Ludlow. 3B. Murchison, B. obtectus, and B. trilobatus are
Upper Ludlow only ; 4 species occur in the Passage-beds, B. cari-
178 PROCEHDINGS OF THE GEOLOGICAL SOCIETY.
natus, B. exepansus, B. Murchison, and B. trilobatus; 6 species
occur in the Upper Ludlow of Westmoreland; Shropshire and
Worcestershire possess 3 of the same species. None are known in the
Ludlow rocks of North Wales, Herefordshire, Scotland, or Ireland.
B. carinatus, B. trilobatus, and B. dilatatus are also Wenlock species.
CrpHaLopopA.—No less than 24 species of Orthoceratites, 6 species
of Phragmoceras, and 3 of Litutes, with other forms, make up the 6
genera and 37 species known in the Ludlow. Ascoceras Barrandii
constitutes a new generic type. The Lower Ludlow has yielded
4 genera, Latuites (3 species), Orthoceras (15 species), Phragmo-
ceras (6 species), and EHxosyphonites (2 species).
The Aymestry Limestone has yielded 3 genera and 6 species—
Tntuites giganteus, Orthoceras 4 species, and Phragmoceras ventricosum.
The Upper Ludlow 5 genera and 22 species—Ascoceras Barrandi,
Litwites giganteus, Orthoceras 17 species, Phragmoceras nautileum,
and Tretoceras semipartitum.
In the Passage-beds we have noted Orthoceras bullatum and Tre-
toceras semipartitum. 16 species of the genus Orthoceras occur in
Westmoreland, mostly Upper Ludlow, and no other genus has yet
occurred there. Shropshire possesses 4 genera and 22 species, em-
bracing most of the species in the Upper and Lower Ludlow divisions ;
Herefordshire 5 genera and 21 species, Ascoceras Barrandu, Intwites
3 species, Orthoceras 11, Phragmoceras 3, Exosiphonites 2. Worces-
tershire has 10 species. Orthoceras Maclareni and O. subgregarium
are the only Scotch forms known ; and O. subgregarium is the only
Irish species. 11 species come from the Wenlock rocks to the Lower
Ludlow, but 16 Wenlock species range through the Ludlow group ;
Ascoceras is the only new genus; and none ranged above wmto erther
Old Red Sandstone, Devonian, or Carboniferous rocks.
Pisces.—No Vertebrata have yet been discovered in earlier rocks
than the Lower Ludlow. Scaphaspis (Pteraspis) ludensis, Salt.,
is the first fish known, and the only species in the Lower Ludlow;
none have yet been detected in the Aymestry Limestone, but every
known Ludlow form occurs in the Upper Ludlow, and five of them
in the Passage- or junction-beds, through which about 20 species of
the Silurian fauna pass to the Lower Old Red Sandstone, 7 of which
are Crustacea (Merostomata), 6 Fishes, and 2 Cephalopoda, &e.
The Crustacea common to the Ludlow and Old Red, and all be-
longing to one order, are Hurypterus abbreviatus, HL. acumimatus, and
E. pygmeus, Pterygotus problematicus, Stylonurus Powriet, S. me-
galops, and Parka decipiens. The fishes that connect the two for-
mations, but only in the Silurian area along the frontier of the Old
Red, are Auchenaspis Salteri, Cephalaspis Murchison, C. ornatus,
Pteraspis Banksii, Scaphaspis ludensis, and Eukeraspis pustuliferus.
All belong to the Ganoidei.
DEVONIAN.
Prant#.—We have no clue as to the region in which the
Devonian Plants first appeared; and yet small as is the flora of
the British Devonian as compared with that of North America it
6éeT
~t i) Ne We tt i) n
x nO OM NY OM Fe oy YY gay PY FA Do we woo From W enlock.
“mojlpvI— ATX aay,
PORYP EP OY OR RE By
ao S, t+ & & 8 SS Gl SS ile ep Ay eo. SS
Spletese | 6D Shy este oO 2 eo =| & = < 1
MEEOne es ce ee UG St Neos ea Sis
Sco Siavces 2 & 2 8 S 5 ©
Vices SS eis: 8 e es 8 8 © s
Moms se Seema Shs Bos os Q
e : © ; © MG s 3 : 5 5 6 —
: Oe Oe ae ke ke ©
wa ee BP: ye
MEE sf eS Pee fe Pk o
: RR RES Bo RoR Sees ;
a "
— ee Se
Sil Sannvoataow Sow BHA oq Genera.
Se lt =A eS eo Tp CO me b> — .
Plea ao SH Hot TH Tw S oxy Species.
DD
No i} _ Ce te pK bt th et ° =F
i bat et one ketiet DODO on® BA oo wo SO ID emo. ao OK AL 0 Lower Ludlow. 2
go
S
: é : try Lime-
ee - OO He ue aN =e bone 5S? Aw wo Oe 5 am ¢ ee =
i )
©
—
ie. _ tS SS om De s) Th = ° Ss
wo | fo Sa on we So TO RE i ER ga se se 5 oa aa | Upper Ludlow. (Se
Ow ° ° Di
De
on
=
36 | OS BS S08 Coy aor Rowse we i 3 5 we | Passage-beds. 2
i= ° e ° e
25 wun ae eet pone a) as ae : Ere OD HH OD + : : | South Wales.
pe] DSH Ef owe am ff we aw nm ee See 2 | North Wales.
i
or by Lo! [al CO et = . | We st 1: d @
ee C at Bre wo KO aK KO nP PR AD AK : Ge 9 estmoreland. ec
| rs
fas)
; ES
2 [me ph SH we Ex Seo So we Sy eu eo Ge om ee eo | Shropshire. Ez.
oe
2 =)
eS Be we 5 wa Zo SY ww SY am on To as ww | Worcestershire. a
| om
=
e ; ae
BS | me Ee we fa Do Bowe Se ae se we non | Herefordshire. °
~ | i
uo | Se pH awe Do of: RE we me aT | Scotland.
nS | ee He wt Bo me won : Oe Treland.
Ne ak Ne OO? DO et
(9)
z
“UVIMOAR(T
0} ssug
180 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
shadowed forth the prolific flora of the Carboniferous epoch, which
in the British Islands numbers 82 genera and 330 species; but the
Devonian, which preceded it, has, up to the present time, yielded
only 12 genera and 18 species. In America, however, about 95
genera and 160 species have been described through the researches
of Dr. Dawson, Lesquereux, Vanuxem, Hall, Hartt, &c., especially
the first-named author, who has devoted a long life to the eluci-
dation of the Devonian and Carboniferous flora of the American
region. 7 of the 12 British Devonian genera occur in America,
viz. Calanuites, Lepidodendron, Psilophyton, Sagenaria, Spheno-
pteris, Stigmaria, and Trichomanites ; but our ill-preserved speci-
mens scarcely admit of specific determination, in fact even their
affinities are often difficult to make out; and the poverty of our
flora is clearly seen from the few species (18) occurring to illustrate
the 12 genera. On such slender evidence it is difficult to conceive
from what area our Devonian and Old Red Sandstone flora was
derived; whether migration took place from Central Europe or
America. The facies appears to be American rather than European,
this being the case with the Scotch and Irish floras, especially
-through Psilophyton, Paleopteris, and Sagenaria.
The Lower Devonian (Lower Old Red) has yielded 2 species,
Lepidodendron nothum, Unger, and Psilophyton Dechenianum, Carr.,
with coniferous remains from Caithness and Wick in Scotland. The
Middle Old Red contains Caulopteris Peachi, Salt. (=? Psilophyton
robustus, Dawson), and the two mentioned as occurring in the Lower
beds. The Upper Old Red species (12) approach closely to the Car-
boniferous. 7 genera and 12 species range through the Upper divi-
sion—Advantites 1 species, Calamites 1, Filicites 1, Sagenaria 5,
Sphenopteris 2, Trichomanites 1, and Anorria 1. Thus only 18
species occur in the widely extended and thickly developed deposits
of the Old Red of Scotland, the Silurian Old Red, and the rocks
of the Irish area.
Prorozoa.—Scyphia turbinata, Spherospongia tessellata, and 5
species of Stromatopora all occur in the Middle Devonian; Cawno-
ora, Phillips, Sparsispongra, D’Orb., and Coscinopora of Goldfuss are
probably synonyms of Stromatopora, The Middle Devonian lime-
stones of Torquay and Newton Abbot abound in the ever-varying
forms of these incrusting Protozoa. The Devonian forms differ
essentially from the Wenlock and Ludlow species, the type in those
rocks being S. striatella, whereas the characteristic species in the
Middle Devonian are S. concentrica, Goldf., and S. placenta, Lonsd.,
or the Caunopora of both Phillips and Lonsdale. No Protozoa occur
either in the Lower or Upper Devonian, being strictly confined to
the massive limestones of South and North Devon. S. placenta, S.
ramosa, and S. verticillata are strictly British.
Actinozoa (Actinoidea, Dana; Coralliaria, M.-Kdw.).—Perhaps
during no period in the physical history of the British Islands have
we had such a remarkable assemblage of Actinozoa as that which
so essentially and specifically characterizes the Middle Devonian
rocks of South and North Devon. Out of the 24 known genera and
ANNIVERSARY ADDRESS OF THE PRESIDENT. 181
52 species, no single form passes to the Carboniferous, and none are
common to the Silurian rocks in any area; they stand alone, and
are sufficient in themselves to maintain the integrity of the Devonian
system. This is equally definite and distinct throughout the Kuro-
pean or American areas, or wherever the Devonian rocks are deve-
loped. 15 genera illustrate the Zoantharia rugosa and 8 the Z. tabu-
lata. The genus Acervularia numbers 7 species, Alveolites 4, Cya-
thophyllum 12, Favosites 5, Smithia 3, Endophyllum 2, and Petraia 2.
The remaining 18 genera are only represented by 1 species each ; 20
species are common to the rocks of North and South Devon, and 25
occur on the continent (Rhenish Prussia, Belgium, and France) ;
none pass to the Carboniferous rocks in any region. ‘The Lamelli-
branchiata, Gasteropoda, and Cephalopoda are all of equal strati-
graphical value. The Middle Devonian group contains all the 24
genera and 48 of the 52 species. The Lower Devonian has hitherto
only yielded 4 genera and 7 species; the latter are Alveolites sub-
orbicularis, Cyathophyllum helianthoides, Petraia celtica, P. gigas, P.
pleuriradialis, P. bina?, and Pleurodictyum problematicum ; and the
Upper Devonian also 4 genera and 7 species, viz. Amplexus tortuosus,
Cyathophyllum cespitosum, C.ceratites, Pistulipora eribrosa, Michelinia
antiqua, Petrara celtica, and P. pleuriradialis. The researches of Dr.
Nicholson upon the Devonian Corals of North America have thrown
much light upon their history, habits, and mineralization ; and itis
to be hoped that his labours will be embodied in a volume upon the
Rugose Corals, equal in interest and value to his late contribution on
the Tabulata. Doubtless the Paleeozoic Actinozoa of the British
rocks now require critical revision, especially the Silurian and Car-
boniferous groups.
The Upper and Lower Devonian rocks are chiefly composed of
slates, with here and there impure limestones. They therefore
possess no coral fauna; whereas the highly developed masses of
limestone around Torquay and Newton Abbot are simply Devonian
coral reefs of great magnitude. In North Devon, between Lfra-
combe and Linton, the limestones are lenticular, thin, and im-
pure; yet more than one half of the entire known Devonian Acti-
nozoa have occurred in them, and we have evidence of beds below
at low-water level near Llfracombe yielding even finer specimens
than at Torquay. They have to be searched for in North Devon
and West Somerset ; patient working over that extensive area be-
tween Barnstaple and the Foreland with unbiassed views and a
knowledge of the fauna which exists altogether independent
either of the Silurian or Carboniferous, would readily convince
those who have never examined the county that the rocks of North
Devon between Baggy and the Foreland have nothing whatever to do
with theCarboniferous system. ‘The fossils alone, setting aside strati-
graphical evidence and succession, determine the relation of this
area to Belgium, the Rhine, and France; and their continuity under
Somersetshire, Wiltshire, Berkshire, and Middlesex on to the continent
is no longer matter of doubt or speculation, for the philosophical
and far-seeing views and hypotheses of Mr. Godwin-Austen and Prof.
VOL. XXXVIL. 0
182 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Prestwich have been fully realized, through the determination of
the Devonian and Silurian rocks in Middlesex and Hertfordshire,
immediately below the Cretaceous series.
EcHINopERMATA.—/ genera of Crinoidea, 2 Asteroidea, and 1
Blastoid are all that are known of this class in the British Devo-
nians. 80 genera have been described from the Devonian rocks of
Europe and America. By comparison, therefore, the British fauna has
scarcely any claim to recognition, and 5 of the 7 Crinoidea are also
Carboniferous in Britain. It cannot be said, therefore, that the species
in this division of the order are representative in Britain. The 10
genera and 24 British species are of necessity unequally distributed.
Actinocrinus tenwmstriatus, Phill., Cyathocrinus megastylus, Phill.,
and C. pinnatus, Goldf., are the only forms known in the Lower
Devonian ; 6 genera and 12 species occur in the Middle Devonian,
viz. Actinocrinus 1 species, Cupressocrinus 2, Cyathocrinus 3, Hexa-
crinus 3, Platycrinus 2, and Taxocrinus 1 species.
The Asteroidea all belong to the upper division, and are mostly
from the North-Devon beds, which with them have also yielded 7
Crinoidea. We have therefore 8 genera and 14 species in the Upper
Devonian beds of North Devon—Protaster 2 species, Paleaster 2,
Helianthaster 1, Pentremites 1, Adelocrinus 1, Actinocrinus 1, Cyatho-
crinus 5, and Taxocrinus 1 species. Of the whole fauna (24 species)
3 genera and 6 species pass to the Carboniferous; they are Actino-
crinus triacontadactylus, Cyathocrinus ellipticus, C. geometricus, C.
pinnatus, C. variabilis, and Pentremites ovalis. Three of these are
European Devonian.
AnnELIpa.—Serpula advena, Salt., occurs in the Upper Old Red
Sandstone of Caldy Island, and Yentaculites annulatus?, Schloth.,
in the Middle Devonian of North Devon; the last named is abundant
(in places) in the limestones near Ilfracombe.
CrustaceA.—All the 4 orders, illustrated only by 20 genera and
37 species, are represented in the British Devonians ; 45 genera and
290 species, however, have been described from Bohemia, Germany,
Spain, Asia, Africa, America, &c. 20 of the foreign genera and 200
species are Trilobita ; the remaining 90 are Merostomata, Phyllopoda,
and Ostracoda. As in the case of the Echinodermata our Crustacean
fauna is any‘thing but representative, yet it has a characteristic
facies that carries with it the conviction of distinctness. Only 6
genera of Trilobita are known, viz. Bronteus (flabellifer), Cheirurus
(articulatus), Harpes (macrocephalus), Homalonotus (elongatus), Pha-
cops (Sspeciesincluding the subgenera 7rimerocephalusand Crypheus),
and Phillipsia (Brongniarte); the doubtful genera have been relegated
to their supposed places. 9 genera and 24 species of all the orders
are Lower Devonian (6 genera are Trilobita), 5 genera and 6 species
are Middle, and 7 genera and 9 species are Upper Devonian.
Eurypterus (6 species), Stylonurus (6 species), and Pterygotus (4
species) are all, with one or two exceptions, Lower Old Red Sand-
stone types. None of these are known to occur in the typical Devonian
area, being either Scotch or in the Silurian region. The singular
genus Prearcturus (P. gigas, Woodw.) of the family Idoteide is
ANNIVERSARY ADDRESS OF THE PRESIDENT. 183
from the Old Red of Herefordshire; this and Proricaris M‘Henrici
of Baily form the only 2 new British genera introduced into the
Devonian fauna. Phillipsia Brongniartii is the only crustacean that
occurs in common in the Devonian and Carboniferous rocks ; it is the
Asaphus obsoletus and A. granuliferus, Phill.; so that, small as the
Devonian Crustacean fauna appears to be, it is nevertheless distinc-
tive. A. Romer, Sandberger, Dalman, Brongniart, Richter, Minster,
Beyrich, Steining, Roualt, &c. on the continent, with Salter, Phillips,
Woodward, Jones, R. Etheridge, jun., and Baily in Britain, have all
greatly enriched our knowledge of the Devonian Crustacea.
Bryozoa.—The Tubuliporide through Ceriopora, the Retioporide
through Henestella, Henntrypa, Polypora, Ptylopora, and Retepora,
and the Hscharide through Glauconome, are represented through the
Devonian rocks by the above 7 genera with 11 species; all the
genera are equally Carboniferous, but only 4 species are common to
both formations-—Ceriopora similis, Phill., Fenestella plebeia, M‘Coy,
Glauconomne bipinnata, Phill., and Polyporalaxa,Sandb. The Lower
Devonian possesses 2 species only, viz. Henestella antigua, also oc-
curring in the Middle and Upper, and Retepora repisteria, which is
also Middle Devonian. 6 of the 7 genera and 7 species are Middle
Devonian—Polypora, through its representative species (P. lawa),
being Upper and Carboniferous. 5 genera and 6 species are Upper
Devonian ; they are both South- and North-Devon forms—Cerio-
pora (Millepora) gracilis, Phill, Fenestella antiqua, Goldf., F.
prisca, Goldf., #. plebera, M‘Coy, Glauconome bipinnata, Phill.,
and Polypora lava. The known Devonian Bryozoan fauna (Kuro-
pean, American, and British) consists of 26 genera and 115 species ;
of these we have only 7 genera and 11 species. These species
range through North and South Devon and South Cornwall; they
are rarely well preserved and always difficult to determine. Critical
analyses of the species have been undertaken by Messrs. Shrubsole
and Vines, who in time will revise the entire group.
Bracuropopa.—With the exception of the fishes of the Old Red
Sandstone (125 species) this is the largest group in the British
Devonian rocks. We should expect this when we know that no
less than 61 genera and over 1100 foreign species have passed
through the hands of European, American, and British zoologists and
palzontologists, and all have been described ; of these 1100 species
only 116 are British; and of the 61 known genera we possess 26.
Calceola (1), Davidsonia (3), Cyrima (A), Rensseleria (11), Camaro-
phoria (1), Stringocephalus (1), and Uncites (1) are the genera new to
Britain, none of which made their appearance in our area until the
Middie periodof the Devonian deposits, the most marked and prolific
of the three horizons. With the exception of Cyrtina, which exhibits
_4 species, each of these genera is represented only by 1 species.
Hall’s genus Rensseleria yields 10 as the total value of the genus ;
but only 1 species occurs in Britain (Rensseleria stringiceps, Rom.) ;
8 of the rest are American, and 1 species is Coblentzian. JI call
attention to these 7 genera because they are essentially Devonian ;
the remaining 19 appeared in the Silurian rocks, and lived on
through the Carboniferous.
02
184 PROCEEDINGS OF THE GEOLOGICAL SOCINTY.
The Lower Devonian yields 9 genera and 21 species—Athyris 1,
Atrypa 3, Chonetes 3, Leptena 1, Or this 3, Rhynchonella 3, Spirifera
3, Spur iferi ina 1, Sér eptorh ynchus 3. The Middle division contains
23 genera out of the 26, and 80 of the 116 species. The Upper
contains 14 genera and 37 species; of these 10 genera and 16
species pass to the Carboniferous. It is essential to the history of
the Devonian fauna that I name the genera—Athyris 2 species, Cho-
neétes 1, Discina 1, Lingula 1, Productus 1, Rhynchonella 3, Spirifera 3,
Streptorhynchus 1, Strophomena 1, Terebratula 2. The large genera
are Lthynchonella 16 species, Spirifera 20, Streptorhynchus 6, Orthis
6, Cyrtina 4, Productus 4, and Terebratula 4. Regarding the
great discrepancy or smallness of this peculiar fauna as compared
with that of the continent and America, we must have regard to the
smallness of the area now exposed in England as compared with the
original area occupied by the Devonian sea, the accumulations of
which are now covered by the Secondary and Tertiary rocks of the
west and east of England, the Devonian floor or old surface being
hidden east of the Quantocks, North Devon, and Torquay. We have
proof of a rich Upper Devonian fauna in the rocks under London
and Turnford, at the depth of 1000 feet, and below the Cretaceous
series ; between these two places and North Devon we can at pre-
sent only surmise the plane they occupy.
The volume of the Paleontographical Society’s publications by
T. Davidson, Esq., F.R.S., &c., devoted to the British Devonian
Brachiopoda, is worthy of the fame of its distinguished author; in it
are described 116 species, the arguments for and against their
genuineness being impartially and consummately reasoned out,
figures of all the species and doubtful forms are given; and when
we know the patience and skill required to adjust and discriminate so
dismembered and small a group as the British Devonian Brachiopoda
out of such a mass of material occurring in the European and Ame-
rican fauna (1100 species), we may well be thankful that there are
men who have the required leisure and knowledge and who devote
their lives to one subject. Associated with Davidson in the Devo-
nian fauna, the names of Von Buch, Schlotheim, Schnur, Dalman,
Sandberger, Hall, Billings, Dall, Conrad, Romer, Vanuxem, Bar-
rande, De Verneuil, Roualt, Phillips, Sowerby, King, and M‘Coy
must be prominently noticed.
LAMELLIBRANCHIATA.—The mass of the species of the class Conchi-
fera occurring in the Upper Devonian, and especially abundant,
are Asiphonida, through Avieulopecten, Pterincea, and the Mytilidee.
20 genera and 39 species are known, and 29 species illustrating 11
genera are in the Upper division ; yet of the whole bivalve fauna
only 4 genera and 5 species pass to the Carboniferous series in
North Devon, viz. Aviculopecten granosus, Sow., A. plicatus, Sow.,
Pterinea damnonensis, Sow., CuculleaGriffithu, Salt., and Curtonotus
unio, Salt. The Lower Devonian is even poorer, only 3 genera and
4 species occurring; these are Aviculopecten polytrichus, Phill.,
Pierinea anisota, Phill., P. spimosa, Phill., and Otenodonta Kratche,
Rom.; the last mentioned is the only bivalve species actually con-
ANNIVERSARY ADDRESS OF THE PRESIDENT. 18 5
fined to the Lower Devonian. ‘The Middle Devonian is represented
by 13 genera exhibiting 23 species—<dviculopecten 2 species, Péeri-
nea 6, Anodonta Jukes, Cledophorus ovatus, Corbula Hennahe,
Cucullea Hardingu, C. trapezium, Ctenodonta lineata, Leptodomus
constrictus, Megalodon 3, Modiola scalaris, Pleurorhynchus 2, Pul-
lastra antiqua, and Sanguinolaria elliptica. Megalodon, Pleurorhyn-
chus, Corbula, and Clecdophorus are generically and specifically essen-
tially Middle Devonian. Cucullwa 6 species, Curtonotus 6, Cteno-
donta 4, are the larger genera of the Upper Devonian beds of North
Devon, south of the latitude of Baggy Point; but we have seen how
few pass to the Carboniferous south of Barnstaple and Pilton, or along
the strike of the two formations from Barnstaple to Braunton. The
South-Petherwin and Land-lake beds in North Cornwall are Upper
Devonian, and have yielded 65 species ; they cannot be affiliated with
the Carboniferous, the Clymenie and species of Orthoceratide for-
bidding it.
Any comparison of the insignificant British fauna with the splendid
series of Devonian species in Kurope and America is useless : no fewer
than 90 genera and 900 species of Lamellibranchiata have been de-
seribed ; 260 are Monomyarian and 640 are Dimyarian species.
GasrEropopa.—13 British genera and 45 species constitute the
entire list of the Odontophora. No species occurs in the Lower Devo-
mian. ‘The Middle, as in the case of all the other classes, contains the
largest number of species (36) and 12 of the 13 genera—Acrocula
3 species, Huomphalus 5, Lowonema 5, Macrocheilus 6, Murchisona 4,
Nerita 1, Pleurotomaria 6, Scoliostoma 1, Trochus 1, Turbo 2, and
Vermetus 2 species. The Upper Devonian species are 14, and occur
mostly in the Pilton, Brushford, and Petherwin areas; they represent
7 genera—Aecroculia 1, Huomphalus 1, Loxonema 4, Macrocheilus 1,
Murchisona 1, Natica 2, and Pleurotomaria 4. 5 species pass to the
Carboniferous—Acroculia vetusta, Lovonema rugiferum, L. tumidum,
Murchisoma angulata, and M. spinosa.
The South-Devon area has yielded 37 of the 45 Middle Devonian
species, North Devon only.5, viz. Huomphalus serpens, E. radiatus,
Acroculia vetusta, Macrochelus brevis, and Natica meridionalis,
and 11 Upper Devonian ; the Petherwin beds in North Cornwall
contain 7 Gasteropods, all Upper Devonian. Complete comparison
of the two areas will be made at the end of the Devonian fauna.
Preropopa.—No Conularia or Theew has appeared in the Devonian
rocks of either South or North Devon. 30 species are known in
the Devonian rocks of Germany and America.
Hureropopa.—The order Nucleobranchiata through the Atlantidee
is represented in all three divisions of the Devonian rocks by Belle-
rophon (5 species) and Porcellia (3). Bellerophon bisulcatus occurs in
the Lower and Upper divisions; B. striatus, Lower and Middle;
B. hiulcus, B. subglobatus, and B. Urii in the Upper; B. hiulcus and
B. Urii appear also in the Carboniferous rocks. B. subglobatus is also a
Coomhola species (Irish). Porcellia Woodwardi, Sow., and P. striata,
Phill., occur in the Middle Devonian of South Devon; but P. Symondsiz
has hitherto only been found in the Upper division, or Pilton and Barn-
186 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
staple beds south of Baggy. Thus these 2 genera and 8 species have
a wide range, due to their pelagic habit; and regarding B. Uri, B.
hiulcus, and B. subglobatus as Carboniferous, 3 occur in the Lower,
3 in the Middle, and 5 in the Upper Devonian. 5 genera and 77
species are Continental and American.
CrpHatopopa.—Clymenia, Cyrtoceras, Goniatites, Nautilus, Ortho-
ceras, and Poterioceras are the 6 British Devonian genera with 60
species. Other foreign genera and 500 species are noma We can
hardly attempt comparison through such an extensive and widely
disseminated group. (The genus Goniaiites is illustrated by 168
species, Clymenia 50, and Orihoceras 130; but Bactrites with 9
species, Cyrtoceras 60, Phragmoceras 12, and Trochoceras 6 species,
are not known in the British Devonians, besides many other smaller
genera.) Strange as it may appear, only one species occurs in the
Lower Devonian, Cyrioceras bdellahies, Stutchb.; yet this genus is
represented by 12 Middle and 2 Upper Devonian species. I am
disposed to believe that we have not in Britain any Lower Devonian
form at all, this single species from one locality being doubtful.
The 11 other forms are all Middle Devonian.
Clymenia, the essential genus in the Devonian rocks of Britain
(and elsewhere), numbers 11 species, and all occur in the Upper
Devonian of Petherwin in North Cornwall. This genus is repre-
sented in Europe by 50 species, and, in the same stratigraphical
position, in the Upper division of the Devonian serics. America
yields scarcely any Clymenie; and no Clymenia occurs in the Devo-
nian rocks of North Devon, either Middle or Upper.
Gonratites—In the Upper Devonian of Petherwin this genus is
represented by G'. biferus, G. linearis, G. subsuleatus, G. striatus,
and G. vinctus; and 12 species occur in the Middle Devonian of
Torquay ; only 2 forms occur in the Upper beds of North Devon,
G. vinctus and G. spirorbis; 4 of the Devonian species occur in the
Carboniferous rocks, G. carbonarius, G. cxcavatus, G. serpentinus,
and G. subsuleatus? As compared with the Carboniferous Gonia-
tites, the Devonian group is of slight importance ; in Britain alone
we have 72 Carboniferous species, and 160 Devonian species have
been described from European rocks, and only 6 or 8 from America.
Cyrtoceras—— With one exception the 15 species of this genus
occur only in the Middle Devonian of Torquay. The single departure
from this is Cyrtoceras rusticum, the only Upper Devonian form in
the Petherwin beds ; this species is probably the C. arcuatum of Stein-
meyer. 60 species occur in the Devonian rocks of Central Europe ;
and, as in the two genera before noticed, few are American.
Orthocer as.—No species of Orthoccras has yet occurred in the
Lower Devonian beds, either of North or South Devon. The Middle
group at Torquay has yielded 8 species, and the Upper Devonian of
North Devon 13 ; and 4 of these North-Devyon species pass to the Car-
boniferous south of Pilton and Barnstaple, viz. O. cinctum, O. lineola-
tum, O. striatum, and O. undulatum. 130 species occur in the Deyo-
nian rocks of Rhenish Prussia and Central Europe, and less than 20
in America. Our Carboniferous rocks contain 47 species; but, as we
have seen, only 4 species are common to the two formations.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 187
Nautilus.—The European area, so rich in the 4 genera previously
noticed, is unexpectedly poor in Nautilz, not more than 11 species
haying been described therefrom, and only 4 or 5 from America.
We possess only 2 species, VV. germanus and NV. megasipho; the
former Middle Devonian, Torquay, the latter Upper Devonian, from
Petherwin.
Poterioceras.—Only in the Upper beds at Petherwin is this genus
represented, and by 1 species (P. fusiformis) ; it also passes to the
Carboniferous rocks. The analysis of the Devonian Cephalopoda and
their distribution show that the British species number 60, belonging
to the 6 genera I have separately discussed. Only 1 is Lower Devyo-
nian ; the Middle Devonian has yielded 4 genera and 33 species, and
the Upper 5 genera and 33 species.
Looking, then, at our small Devonian Cephalopod fauna (6 genera
and 60 species) as compared with that of Europe (20 genera and 500
species), which alone nearly equals all the species in the 14 classes
in the British Devonian rocks (544), we readily see the value of
this fauna in Europe, Belgium, the Eifel, the Harz, Saxony,
the Fichtelgebirge, Russian Poland, Russia in Europe, and Spain.
In Belgium, France, the Hifel area, the Fichtelgebirge, and Saxony,
the Devonian group, as with us, readily falls under the 3 divisions of
Lower, Middle, and Upper, andin the main the grouping corresponds
or may be correlated with ourown. In Belgium (south of the Condros)
the Psammite of Condros, the schists of Famenne, and the limestone
of Frasne are the equivalents of our Upper Devonian as exhibited
at Petherwin in North Cornwall, and the Baggy, Pilton, Brushford,
and Marwood beds. ‘The ‘“ Givet Limestone” at the summit of the
Middle group is the equivalent of the Stringocephalus-beds of North
Devon, but with us stratigraphically lower.
The Calceola-schists and the (Spirifer) “ Cultrijugatus-Stufe ”
of Belgium are our Calceola-beds of Torquay and Newton in South
Devon, and the typical Middle Devonian. The schists of Burnot,
Ahrian, and the Coblentzian and Gadinian correspond with the
Tinton and Lower slates and grits of North Devon—our Lower
Devonian (the lowest probably not seen). In the Eifel area, the
beds of which, like the deposits of Belgium, correspond so closely
with our own, the Goniatite-schists and (Rhynchonella) Cuboides-
limestone are, like those of North Cornwall and Devon, the upper
division; and, as in Belgium, the Calceola-schists and Cultrijugatus-
Stufe are the equivalents of the South-Devon limestones or Middle
Devonian: the Vichter schists, Ahrian (of Dumont), and the Coblentzian
beds represent the mass of the lower shales, slates, and grits below
the Hangman beds in North Devon. M. Gosselet*, in his succession
of the Devonian rocks of North France and Belgium, divides the
whole into 6 divisions or beds. The corresponding North-French
beds to our Upper Devonian are probably the Psammites of Condros,
the slates of Famenne, and the Boulonnais beds.
The Givet Limestone and;Calceola-slates are our Middle Devonian,
and the systeme Rhénan the Lower.
* Bull. Soe. Géol. de France, vol. xviii. p. 18.
188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
M. Gosselet* again divides the Devonian of the Franco-Belgian
region into Upper, Middle, and Lower, but with differences which
have paleontological value.
His Upper Devonian contains the Psammites du Condros in 2 divi-
sions; the Schistes de Famenne in 4 divisions.
The Middle Devonian one large group (caleaire de Givet) divided
into 9 beds or bands.
In the Lower Devonian Gosselet places (1) the schistes & Calecoles
(in 3 divisions), (2) Poudingue de Burnot, (3) the Grauwacke 4
Leptena Murchisoni (in 2 divisions), (4) the Couches de Gedinne and
conglomerates and schists (in 3 divisions).
In the departments of the Loire Inférieur and Maine-et-Loire,
according to M. Caillinaud, the Lower Devonian occupies large areas
in the west of France; and in the same departments M. Bureau
has determined the presence of the Upper Devonian.
In Rhenish Prussia, in the Eifel district, the Devonian strata were
long studied by Ferd. Romer, of Breslau, and Dr. Emanuel Kayser.
They determined the following horizons and successions f :—
MherGonvatitelschists ) esses. ee
Cuboides (Rhynchonella) limestone ... Marly limestone, (Uo ee
Stringocephalus-schist
Calceola- schists ie pean hy cre ec inerene Marl, Middle Devonian.
Cultriyjugatus-Stufe (Spirifer)
Vachteriscistee teri ene cca
Ahrian schist (Dumont) ............... Sandy schists, Lower Devonian.
Coblentzian iia ae ere een ee
eeeeeesecsecesrese
F. A. Romer, of Clausthal, has correlated the parallel horizons or
deposits of the Harz and the Eifel. In the Hifel he gives 7 divisions,
in the Harz 8; they are compared with Aix-la-Chapelle and Couvin.
In the ‘ Paleontographica’ (for 1854), F. A. Romer divides the
Devonian rocks of the Harz into 9 portions :—
. Amay schists (jiingere Grauwacke),
. Cypridina-schist.
. Goniatite-schist.
. Iberg limestone.
. Receptaculites-schist.
. Stringocephalus-limestone.
. Orthoceratite or Wissenbach schist.
8. Calceola-schist.
9. Spirifera-sandstone (altere or Rhenish Grauwacke).
Characteristic fossils are given with each, and the chief localities
where the beds are exposed. F
The Fichtelgebirge, through the researches of Prof. C. W. Gumbel,
exhibit 4 divisions or groupings :—
JWoOuUp WN eH
1. Cypridina-schist......... Upper Devonian (in 3 stages).
2. Calamopora-schist ...... ere re
3. Tentaculite-schist ...... J tibelally Dereuten
4, Nereite-schist ...........- Lower Devonian.
* Annales des Mines, 6° sér. tom. xii. p. 595.
+ Zeitschrift d. deutschen geol. Gesell. Jahrg. 1871, p. 375. bang
t ‘Paleontographica,’ Dunker and Meyer, x1. p. 109, “ Ueber Clymenien in
den Uebergangsbilden des Fichtelgebirges.”
ANNIVERSARY ADDRESS OF THE PRESIDENT, r89
I have thus referred to some of the chief European localities and
systems to show the importance and development of the continental
Devonian rocks with their enormous fauna, as compared with the
clearly determined but comparatively poor British series, our whole
fauna only numbering 550 species at most. Unless some reference
had been made to the American and European Devonians no force
could have been given to the system; and its geographically dis-
jointed state (even on the continent) tends to detract from the original
unity of the whole, but at the same time to show that it was,
and has been, one of the most extensive systems on the two conti-
nents, and even in the British Islands could we but uncover the
extensive area between Belgium, the Boulonnais, and Devon and
Cornwall, now deeply buried under the Secondary and Tertiary
systems.
I cannot pass over the Devonian formation of North America
and the Canadas, either physically or paleeontologically, for we know,
through the labours and researches of Hall, Bigsby, Newberry,
Meek, Shumard, Winchell, Dawson, and others, how great and widely
extended is the Devonian system in North America, and how persistent
are the conditions and successions; the state of New York and the
Canadas, with the Gaspé region in the east, have as yet exhibited
the Devonian rocks in greatest development, all the three great
horizons being present. The Hamilton and Upper Helderberg
groups, with the Catskill, Chemung, and Portage groups above,
occur in the States of Pennsylvania, Ohio, Llinois, Missouri, and
Michigan in full development. In lowa and Tennessee the Upper
Devonian only is present. In New-York State the 11 recognized
divisions make up a mass of limestones, sandstones, shales, flag-
stones, and conglomerates upwards of 8000 feet in thickness. In
Pennsylvania the Devonians are 12,000 feet thick. The great
Middie or Hamilton group is developed in 6 of the 8 States, the
Lower or Helderberg in 4. Principal Dawson, in his ‘ Acadia,’ has
shown that the Devonians of the St.-John’s area, New Brunswick,
exhibit peculiar features different from those of the Western States
before mentioned, but nevertheless are divisible into three stages
or horizons*.
The above generalizations relative to the development and dis-
tribution of the European and American Deyonians are given to
show their great value and extent as compared with the really
or comparatively poor fauna of the British Islands. That the whole
formation or system once extended universally over the area thus
roughly traced there cannot be any doubt, nor that probably during
one general age one or other of its three divisions may have occurred
homotaxially ; but as a whole it occupied all that time or epoch
extending from the close of the Upper Ludlow to the base of the
Carboniferous. In North Devon its upper member passes insensibly
and conformably into the Carboniferous, which is itself in an abnormal
eondition.
The Scotch and Irish beds of this age differ from all others, the
* © Acadia, 2nd ed. pp. 503-505.
Igo PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Trish Coomhola beds, with Anodonta and Paleopteris or Adiantites,
being undoubtedly of Upper Devonian or Upper Old Red Sandstone:
age. Mr. Kinahan would class the Old Red Sandstone of the
Dingle and Cork area as Lower Carboniferous, and corresponding
in the Limerick area to the Lower Carboniferous sandstones and
shales. Kinahan further states that in no place in Ireland has
the Old Red Sandstone a defined upper boundary, one group gra-
duating into the other. Furthermore, he says, only in Munster
and in the hills between Lough Erne and Pomeroy, in the counties of
Fermanagh and Tyrone, is the Old Red Sandstone at the absolute
base of the Carboniferous formation, as in all other places the
rocks so called and described are on different geological horizons,
ranging up to the base of the Coal-measures*.
As far back as 1863 Jukes and Salter stated that the yellow lime-
stone of the South of Ireland is the upper part of the Old Red Sand-
stone, with the Coomhola grits between it and the Carboniferous
slate with Avicula damnoniensis and Cucullea &e.
Piscrs.—50 genera and 125 species of fish range through the
Old Red Sandstone. It can hardly be said that ichthyic life com-
menced prior to the commencement of the deposition of Old Red Sand-
stone or the Devonian age. The few genera and species that made
their appearance in the British seas at the close of the Silurian
period (8 genera and 12 species, 10 of which passed to the Old Red
Sandstone) can only be traced into the very lowest beds of the Old
Red in the Silurian area of Ludlow, Kington, and Ledbury, and
scarcely passing beyond the passage group; we know them not
higher in the system. Inthe North of Scotland and in the Orkneys,
Caithness, and Cromarty area, the Lower Old Red Sandstone is
known to have furnished 18 genera and about 60 species ; no prior
stratigraphical relation or origin is known. They occur in that
region, like the strata or rocks which contain them, fully developed
and in vast numbers. Unlike the Old Red Sandstone of the Silu-
rian area the formation has there no fossiliferous base. ‘The Silurian
rocks are absent, the sandstones and conglomerates lying uncon-
formably upon the metamorphic rocks. The only other organisms
are Phyllopod and Eurypterid Crustacea, with remains of 10 or 11
genera of plants.
To no living geologist are we so much indebted for our intimate
knowledge of the Old Red of Scotland as to Prof. A. Geikie. His
paper in the ‘ Quarterly Journal of the Geological Society’, on the
Old Red Sandstone of the South of Scotland, and his last elaborate
essay upon the Old Red Sandstone of Western Europe, are ex-
haustive so far as they have gone. Prof. Geikie shows that there
is no middle Old Red Sandstone in either North or South Scotland,
* Vide Kinahan, ‘ Geology of Ireland,’ pp. 50-94, for his views and much
valuable information.
+ “On the Old Red Sandstone of the South of Scotland.” By A. Geikie, Kisq.,
F.G.S. Quart. Journ. Geol. Soe. vol. xvi. pp. 312-328.
t+ “The Old Red Sandstone of Western Europe.” By A. Geikie, LL.D.,
F.R.S. Trans. Roy. Soc. Edinburgh, vol. xxviii. 1878.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 1gt
but that it consists only of two great divisions—a lower, passing down
conformably into the Upper Silurian shales, and an upper, graduating
upward into the Lower Carboniferous sandstones, with a complete
discordance between the two series.
Prof. Geikie in his memoir traces the series of changes in the
physical geography of Western Europe which took place between
the close of the Upper Silurian and the commencement of the Car-
boniferous period. Viewed in a large sense the Old Red Sandstone
of Great Britain groups itself stratigraphically into two divisions,
physically and paleontologically distinct, a lower and an upper.
Prof. Geikie regards the Old Red as a great lacustrine accumula-
tion, and treats of the separate basins of deposit as lakes, to which
he has assigned different names :—
1. Lake Orcadie.-—* Kmbracing all the Old Red Sandstone to the
north of the Grampian range, including all the Orkney
Islands.”
2. Lake Caledoma or the Mid-Scottish Basin.—* Occupying the
central valley of Scotland between the range of the High-
land mountains on the north and that of the Silurian
pastoral uplands of the southern counties. This basin was
probably prolonged across the Firth of Clyde into the north
of Ireland.”
3. Lake Cheviot.— A portion of the south-east of Scotland and
the north of England, extending from near St. Abb’s Head
south-west along the base of the Silurian hills to the head of
Liddesdale, and including the area of the Cheviot Hills.”
4, The Welsh Lake.—‘ The Old Red Sandstone region of Wales,
bounded on the north and west by the Cambrian and Silu-
rian rising grounds, but its eastern and southern extension
obscured by later formations.”
Lake of Lorne-—*“ A district in the North of Argyllshire ex-
tending from the south-east of Mall to Loch Awe, and
perhaps northward up the line of the great Glen.” |
Ca
OV
At p. 374 of his memoir Mr. Geikie gives the order of succession
among the strata, the thickness, and typical localities of the Old Red of
Caithness, which he makes 16,200 feet thick, and then treats of all
the subdivisions separately. Pp. 406-414 treat of the Orkney
Islands paleontologically and physically; and pp. 414-421 of
the Shetland Islands in the same manner. The description of the
Basin of the northern Firths occupies 26 pages.
I commend this great addition and acquisition to the history of
the Old Red Sandstone of Scotland to every student of geology.
Professor Hull has lately ably discussed the vexed question of
the geological relations of the rocks of the south of Ireland to those
of North Devon and other British and continental districts*.
Mr. Hull had previously discussed, in his paper upon the Dingle
beds and Glengariff grits and slates, the relations of the Upper
* Quart. Journ. Geol. Soc. vol. xxxvi. pp. tell (1860).
Tt Quart. Journ. Geol. Soc. vol. xxxv. pp. 699-728
ig2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Silurian series of the south-west of Ireland to those of the Silurian
region of Engiand, and also the relation of the Old Red Sandstone
to the Dingle beds, and shown that, as in the north of Scotland,
all through the south and centre of Ireland the Old Red is every-
where unconformable to the rocks on which it reposes, while it
passes up conformably into the Carboniferous series.
Prof. Geikie has suggested that the Dingle beds or Glengariff
grits may represent the Old Red Sandstone of Scotland (Joc. cit.).
Should this be the case they would be the marine representatives
of lacustrine deposits. Both, according to Mr. Hull, are uncon-
formably overlain by Upper Old Red conglomerate and sandstone.
Mr. Ralph Tate held the view that the Dingle beds are the
equivalents of the Tilestones or Passage-beds of England and Wales*,
or the lowest Old Red. Prof. Hull endeavours to show that between
the Glengariff beds and the succeeding formation, be it what it may,
either Ola Red Sandstone or Carboniferous, there is a great blank,
or, in other words, ‘unrepresented time.” This long period Mr.
Hull believes was filled up in the south and south-west of England
and in Belgium by the extensive series known as the “ Middle”
and ‘“‘ Lower Devonian beds,” lying between the “ Foreland grits ”
on the one hand and the “ Pickwell-Down Sandstone ” on the other.
Prof. Hull also believes that ‘“‘while a deep sea, in which were
deposited the Middle and Lower Devonian beds, overspread the
south of England and adjoining continental areas, land conditions
prevailed in the south of Ireland during the same period.”
The analogy between the OJd Red Sandstone of the south of Ireland
and its supposed representatives in North Devon, Belgium, and
Scotland receives critical analysis from Mr. Hull. That author
endeavours to demonstrate that the Middle and Lower Devonian
rocks of North Devon are totally unrepresented in the Irish area, no
correlation being possible above the Foreland beds. I believe no
one who has ever examined the area south of the Pickwell-Down
Sandstone can doubt that the Baggy, Marwood, Croyde, Barn-
staple, and Pilton beds are upon the same general horizon as the
Carboniferous slate and Coomhola grits of Ireland, and that the
Pickwell-Down Sandstones represent the Upper Old Red Sandstone
of the south of Ireland. Both on physical and paleontological
grounds these two groups seem to agree. Although the freshwater
shell Anodonta Jukesit has not occurred in the Baggy or Pilton series
in North Devon, its plant associate, Adiantites (Palwopteris) hibernicus,
has been found in the Baggy beds, or immediately above the Pick-
well-Down Sandstone (Upper Old Red). Ido not despair of finding
the Irish shell in North Devon, especially after its occurrence in
Northumberland in the lowest Carboniferous rocks of that area. We
may well believe that the “ lacustrine ” conditions of the south of
Ireland gave place to marine conditions over the Devonian area
during the same time.
Mr. Hull proposes the following tabulated form as representative
tor two areas, viz. the south of Ireland and North Devon :—
* Weale’s series. Geology. Portlock and Tate, p. 72.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 193
South of Ireland. North Devon.
( Carboniferous Limestone. Carboniferous Limestone.
eee Osrboni- | Carboniferous Slate. Beas beds.
ferous beds. Coomhola Grit and Slate (pas- ST en eae
eos ee Baggy and Marwood beds
\ 8 of ( Cucullea-zone).
Old Red Sand- ( Kiltorean beds. Upcot beds ?
stone or Upper } Old Red Sandstone and Conglo- =Pickwell-Down Sand-
Devonian. merate. stone.
Prof. Hull then enters minutely into the question of the equiva~
lency and relationship of the North-Devon, Lower and Middle
Devonian series to beds, if any, in the South-Irish area. The Irish
Upper Old Red Conglomerate does not appear to have had, in that
area, any immediate predecessor; and Mr. Hull suggests and con-
tends that the unconformity between the Glengariff beds and
the Old Red or Carboniferous beds proves that certain strata are
absent or were never deposited over the South-Irish area. If Mr.
Hull’s correlation be correct, it may possibly follow that the Middle
and Lower Devonian of North Devon may occupy the place of the
missing strata in the south of Ireland. Furthermore, Mr. Hull
regards the Foreland grits and slates (the base of the North-Devon
beds) as representing in part the Glengariff beds, which he believes
to be of Upper Silurian age. The Foreland grits and sandstones, the
recognized base of the Devonian rocks in Devonshire, Mr. Hull would
correlate with the uppermost Silurian or Passage-group of Sir R. Mur-
chison; and he also infers that the great gap which appears to exist
in Ireland between the Glengariff beds and the succeeding Old Red
Sandstone and Carboniferous series was filled up in North Devon by
the Mortehoe slates, the Ilfracombe series, and the Lynton beds, or all
the strata that exist between the base of the Pickwell-Down Sand-
stones and the top of the Foreland grits. Mr. Hull’s views as regards
the representative beds in the south of Ireland, North Devon, and
Belgium are carefully tabulated on p. 266 of the ‘ Quarterly Journal of
the Geological Society,’ vol. xxxvi., 1880, the relations of each group
being given. The Belgian and Boulonnais sections are also referred
to and tabulated. Scotland, through Geikie’s latest memoir (Joc.
cit.), is compared with both areas, Devon and North and South Ire-
land. On page 273 is also given a table of representative forma-
tions for Ireland, North Devon, South Wales, Scotland, and Belgium.
These two contributions, by Professors Geikie and Hull, to the his-
tory of the Old Red and Devonian rocks of Scotland, Ireland in
part, and North Devon have materially added to our knowledge of
their physical history and condition.
The distribution of the 49 or 50 genera and 125 species of fish
through all the known deposits of Old Red in the British Islands
seems to result in there being no middle fish-bearing group, either
in England, Scotland, or Ireland. Only 2 genera and 2 species are
regarded as Middle Old Red, Kiwcephalaspis (Cephalaspis) Agassiz,
Lank., and Holoptychius Murchison, Ag.; but it would hardly
appear that these two species are rightly placed stratigraphically.
r9O4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
On paleontological grounds this fully confirms the most recent re-
searches relative to the absence of the Middle Old Red Sandstone
in Scotland and Ireland, and probably in the Welsh area also.
8 genera and 12 species of Elasmobranchii (Placoidei) range
chiefly through the Lower Old Red—many with only 1 representa-
tive, viz. Byssacanthus, Conchodus, Cosmacanthus, Cienacanthus,
Ctenoptychius, and Parexus; also Onchus with 4 and Ptychacanthus
with 2 species. The remaining 114 species represent 9 families and
41 genera, all Ganoidei :—
Genera. Species.
ies @colacamthanh < Soler. 2 2
2) ePlacodermitS.. 00 ero. 3 10
3. Cephalaspide .......... 15 40
ANeChemolepimmyern sais os 1 4.
Sy, (Cahqnwodbyomeim 44 S66 ooc 8 23
6. Sauredipterimi 9.) cis) a4 3 9
MeN CLEMOGIpLETIMI «oye cr ee see 2 ve
8. Phaneropleurini .......- 1 L
DUNC aria dices lo) ata as cart 6 23
41 114
The Lower Old Red is represented by 36 genera and 85 species,
and the Upper by 15 genera and 25 species; and I know of no
spectes that is common to the Old Red Sandstone proper and the
Carboniferous group above.
Those genera that seem to specially characterize the Upper Old
Red Sandstone, chiefly Scotch, are Actinolepis, Asterolepis, Bothrio-
lepis, Cosmacanthus, Dendrodus, Glyptolemus, Glyptopomus, Holopty-
chius (some species), Homothorax, Lamnodus, Pamphractus, Phanero-
pleurus, and Phyllolepis*. The 2 genera(?) and 2 species (?) in the
so-called Middle Old Red tend also to show, through physical re-
search, that no such grouping exists.
56 genera and 150 species, other than British, have been recog-
nized in Europe and America, but are allied through about 40
genera, or that number is common to all three areas, America, the
British Islands, and Europe.
Of the entire British Devonian and Old Red fauna (544 species)
we have seen that 52 genera and 51 species pass to the Carboniferous.
ft give the number of species in the classes that connect the two
epochs :—
* Dr. Traquair is now engaged in carefully revising and describing the
Ganoid fishes of the Old Red Sandstone. They could not be in better hands ;
few men are so competent to undertake so large a task. Many names are only
provisional.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 1Q5
Genera. Species.
ARUN LTS 2 ek.a, of" lash ma etoeeas 2
PP OLOZOM UO fh sd Iolo: sich acdodet a none pass.
ENG EUMOZO isp. 40s) i scdeusia)eue alors 12
ichimodermata. 6)... 3 6
EATIITCING GY 7 5 ean ey cae nae ene none.
GUISE ACC AE ro 5 Ais oa ci ocnk «uty ay: 1 1
IBIEVIOLORS. 9 SB gle Be oer enre + 4
I ACHTON OMS cre ey suev-yersy a ces 10 16
Lamellibranchiata ........ 4 5
Gasteropoda.. 2... es 3 5
NCR OO arch alee) cre alejet ays ® none.
IEvetenopoda: ..i).).. 70:0. os 5 1 2
Cephalopoda. . py -icussworen<dcesi- 3 9
WBS CORE fe Arc ech tvei sista! ceive ee none.
32 51
It will be seen that, out of the 51 species, the two large connect-
ing groups are the Brachiopoda and the Cephalopoda.
Professor Hull, in May 1880, communicated a paper to the Royal
Dublin Society ‘‘On the Relations of the Carboniferous, Devonian,
and Upper Silurian Rocks of the South of Ireland and those of
North Devon”*; and although resembling his previous paper ‘“ On
the Geological Relation of the Rocks of the South of Ireland to those
of North Devon &c.,” it treats of the subject-matter in a different
light. Prof. Hull enters more into the paleophysical geography of
the south of Ireland and North Devon, as indicated by the relation
of the formations and areas respectively. In the south-west of
Treland, north and south of Dingle Bay, the rock-groups which rise
into high elevations belong to the Dingle beds or Glengariff grits and
slates of Professor Jukes. The lowest beds of the Dingle promontory
do not reach the surface amidst the mountain-ranges to the south of
Dingle Bay.
The Glengariff beds may measure about 10,000 feet in thickness.
There is a total absence of the Old Red Sandstone at the base of the
Carboniferous beds+. Contortions in the Glengariff beds are of earlier
date than the deposition of the Old Red Sandstone or Carboniferous
beds ; this therefore implies that between the Glengariff beds and
the Old Red Sandstone there is a vast amount of wanting strata,
indicative also of unrepresented time—in other words, a wide gap
and “prolonged interval of time actually separates the two formations.
It is the representation or filling up of this gap that Prof. Hull en-
deavours to show through the uninterrupted sequence in the Middle
and Lower Devonian beds of North Devon, or through the whole
series from the lowest Devonian up to the base of the Carboniferous
* Proc. Royal Dublin Soe. vol. i. new series, 1880, pp. 135-150.
t Hull, “ On the Geological Age of the Rocks forming the Southern High-
lands of Ireland,” Quart. Journ. Geol. Soc. vol. xxxv. p. 699 e¢ seg. (1879).
Fa
1g0 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
formation in that area. In no other district do we find evidence to
account for such loss, or beds that can be correlated with those of the
south of Ireland. Mr. Hull tabulates the succession of the Carboni-
ferous and Devonian rocks of North Devon and the south of Ireland,
and endeavours to show their relation and probable contempo-
raneity as follows* :—
North Devon. South of Ireland.
( Harthy limestones, with Posidono- Carboniferous limestone.
| mya (Venn Quarry).
Lower Carboni- 4 Barnstaple slates. Lower Carboniferous slate.
OES Sea: | Pilton beds. Coomhola grits and slates
| Marwood beds ( Cucullea-zone). (with Cucullea &c.).
zy Upcot flagstones. Kiltorcan beds (with Ano-
Pe ee | donta Jukesit).
; leiclvell- Down sandstones. Old Red Sandstone and
conglomerate.
= Mortehoe slates.
Ne Ilfracombe limestone group. Strata absent over the area
a Hangman grits(Martinhoe beds). in the south of Ireland.
eaten vera Lynton shales and limestones.
NA eee Foreland grits (base invisible). Glengariff beds, passing
down into the Upper
Silurian beds.
The above table is probably the true reading of the areas under
notice. This table is followed by a concise description of the North-
Devon formations and their fossils, in descending order, from the
Carboniferous series south of Barnstaple to the Foreland grits. It
is worthy of attentive study; and Mr. Hull has marked with an
asterisk the identification by Mr. Baily of those species also occurring
in the Carboniferous and Coomhola beds of the south of Ireland,
thus showing still further, on paleontological grounds, the rela-
tionship between the now separated, but probably once united,
areas.
Mr. Hull’s views “ that the missing chapter between the Silurian
and the Carboniferous, in the paleontological history of Ireland, is
supplied by the rocks of Devonshire with their marine organisms” 1s
probably near the truth ; and the proportions assumed in the geolo-
gical series by the Devonian rocks “ offers a solution to one of the
problems of Irish geology.”
Professor Hull enters into geographical considerations of a minute
character, to which I must refer, and which bear significantly upon
the relative changes of sea and land from the Silurian to the close of
the Carboniferous period. The successive phases of the physical
conditions are given through four diagrams of the British Islamds on
plate v., which show the relations of land and sea, or elevation and
depression.
He believes that there is only one true Old Red Sandstone in North
Devon, which is represented by the Pickwell-Down Sandstone, and
that the Upper Old Red of Scotland and Ireland is not the equivalent
of the Devonshire marine Devonian strata, which are newer and
* Hull, loc. cit. p. 144.
ANNIVERSARY ADDRESS OF THE PRESIDENT, 197
higher. If Prof. Geikie is right in saying that the Scotch Old Red
Sandstone represents the Irish Glengariff beds, then Prof. Hull may
be right in concluding that the Scotch beds are the lacustrine equi-
valents in time of the marine uppermost Silurian strata, the Upper
Scotch Old Red being the equivalent of the same in Ireland.
TABLE X V.—Devonian.
: a : ;
a 8 Ba | oe
OI gq —
Se EI 5 a eu
ae > e & a
oS Classes. © S © S53
=) 3 n 2) ° 5
Qj oO H mt foal eS
Sen feece me Sees By aae
my O D = = =) py
2 2
ffpitlernitea Weeecewereeese-- 12 18 : 3 12 2
WOCOZOR, <sccsses ca cl son 3 3
Hydrozoa.
* € 4
PNCEIMOZOA) catone sc teeece- 24 52 : ab 5% ql
Wehinodermata......... 10 24 2 eA By 3
E J:\10 0016) 110 ER Sere 2 2 1 1
3 @rustacea ....c..s.00cs.. 20 o7 a F q 7
ROW Z Oa acc ms sencouseos- 7 il Z S ss
3 Brachiopoda............ 26 116 ay 28 a ate
Lamellibranchiata ...| 20 39 + 23 29 3
Gasteropoda............ 13 45 36 14 3
Pteropoda.
a 2
Eleteropoda <.2.5...--.- 2 8 3 3 5 2
suit Cephalopodas.......:..- 6 60 : Se 33 3
A WISCES! © cela cece de HOR 25 ae 2 ae
3G Ol ee 195 544 era 268 Toe BA
Contents: 195 genera, 544 species.
Pass to Carboniferous: 32 genera, 51 species.
CARBONIFEROUS SYSTEM.
We must go back beyond the present decade for new matter
bearing upon the history and distribution of the British Carboni-
ferous species—not that any significant change has taken place in
the nomenclature or division of the groups, but speculative and
philosophical views have been propounded by many authors upon
the distribution and redistribution of the Carboniferous land-
surfaces and their relation to still older areas. No one has con-
tributed more than Professor Hull to the elucidation of the Carbo-
niferous strata in England, Scotland, and Ireland. This is notably
VOL. XXXVII. p
198 -PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
the case with his paper on iso-diametric lines representing the distri-
bution of sedimentary strata as distinguished from calcareous strata —
with reference to the Carboniferous rocks of Britain*, also his paper
upon the evidence of a ridge of Lower Carboniferous rocks crossing
the plain of Cheshire beneath the Trias &c.t Another and equally
important communication was brought by him before the Society
«‘ On the Thickness of the Carboniferous Rocks of the Pendle Range
of Hills in Lancashire, illustrating the author’s views regarding the
South-easterly Attenuation of the Carboniferous Sedimentary Strata
of the North of England”t. This was followed by another paper
entitled, ‘‘ Observations on the Relative Ages of the leading Physical
Features and Lines of Elevation of the Carboniferous District of Lan-
cashire and YorkshireӤ. Prof. Hull again in 1876 still further
enriched the literature of the Carboniferous system through a valuable
and exhaustive paper “On the Upper Limits of the essentially Marine
Beds of the Carboniferous Group of the British Isles and adjoining
Continental Districts, with Suggestions for a fresh Classification
of the Carboniferous Series”’||. I consider these contributions of Mr.
Hull of the highest importance, as bearing upon theoretical geology,
and tending to excite us to closer research and broader views as to the
physical geography and distribution of life during the Carboniferous
period—certainly one of the most prolific during Paleozoic times,
governed by the distribution of land and water or their relations one
to the other, under marine, estuarine, and freshwater conditions.
The nature of sediments, whether physical (such as inorganic
sandstones, clays, and shales) or organic (as calcareous marine or
freshwater limestones and their relation to life during deposition),
has hardly received the attention it demands. Little has been
written relative to these since Dr. Bigsby, in his memorable papers
in 1858-59, entered into the history and nature of the sediments
laid down over the sea-bottoms, and the immediate relations of
animal life to the strata which the fossil remains now occupy. He
made comparisons of the State of New York and Wales for obvious
reasons. Bigsby showed, through his elaborate researches, that,
owing to a determinate law (with few exceptions), the accumulated
‘sediments graduate into each other, clearly seen in Wales, Scan-
dinavia, Russia, and America.” The change in sedimentation usually
takes place slowly and tranquilly, and the majority of life in the
uppermost or terminated section perishes, thus showing that destruc-
tion or change can take place without any marked disturbing force.
This is perhaps more manifest in the accumulation of the Carbonife-
rous strata throughout Britain than probably in any other formation.
The marked difference, yet, on the whole, agreement between the
Scotch and border formations, or the Calciferous Sandstone, north of
* “On Iso-diametric Lines as means of representing the Distribution of
Sedimentary Clay and Sandy Strata as distinguished from Calcareous Strata,
with Special Reference to the Carboniferous Rocks of Britain.” Quart. Journ.
Geol. Soc. vol. xviii. pp. 127-146 (1862).
Loc. crt -volwscxixen ps Will { Loe. cit. vol. xxiv. p. 319.
§ Loe. cit. vol. xxiv. p. 223 (1868).
|| Loc. cit. vol. xxxil. pp. 618-651 (1876).
ANNIVERSARY ADDRESS OF THE PRESIDENT. 199
the Cheviots to the latitude of Burnt Island, and those same strata
south of the Tweed to the latitude of Harbottle and on towards
Rothbury &¢., would seem to be due to comparatively small changes
of conditions; and from the mapping by the Survey, Prof. Hull’s sug-
gestion as to the origin of and difference between the calcareous and
true sedimentary or argillo-arenaceous strata, especially as exhibited
in the Upper Silurian, Devonian, and Carboniferous formations, appear
to be confirmed. Mr. Hull regards the true calcareous strata as dif-
ferent in origin and distribution from the other stratified rocks with
which they are associated,—not, indeed, properly coming under the
term sedimentary, this term being restricted to “gravels, sandstones,
shales, and clays,” the presence of both classes of rock in the same
geological group being no argument in favour of their similarity.
Whenever interstratifications occur the limestones may be regarded as
occupying neutral ground between the respective areas of dispersion
of the sedimentary series. Could it be possible to trace the sources of
the ‘‘sedimentary” strata of any formation on the one hand and of the
limestones on the other, they would be found expanding in opposite
directions, this arising from the difference in the origin of the two
classes of stratified rocks, the calcareous being essentially organic and
the sedimentary essentially mechanical. We may, I believe, regard
the predominance of ‘“‘ sedimentary strata” as highly unfavourable
to the development of calcareous deposits in the same group of
rocks, from the fact of interference with the development of
life.
Looking at the physical geology of Beran prior to the deposition
and distribution of the Carboniferous strata it is probable that “a
barrier of land existed, stretching from Wales eastwards, touching
the southern ends of the South-Staffordshire and Warwickshire
coal-fields, and including the Cambrian rocks of Charnwood Forest.”
This barrier Prof. Hull believes was possibly an extension of
the Scandinavian promontory, stretching across the Irish Sea to
embrace the Cambro-Silurian districts of Wicklow and Carlow, and
dividing the Carboniferous rocks of South Wales, Somersetshire, and
Dean Forest from the coal-tracts of Central and Northern England
and Scotland, the strata on each side belonging to two distinct
systems of distribution; and their origin is therefore ‘ due to two
different sets of oceanic currents ” (Hull).
The correlation of the Carboniferous rocks of Britain and Ireland
is even now a matter of difficulty and of difference amongst
those best able to decide. Even the continuous series between
England and Scotland from the Calciferous Sandstones of Fife,
south of the Cheviot, to the Yoredale series of Durham are most
difficult to correlate—much that has been called Carboniferous Lime-
stone being calciferous in one area and even Yoredale in the other.
The literature of the whole question is scanty and unsatisfactory
in the extreme; and in the construction of my Tables these dif-
ficulties have met me everywhere. The wide difference that exists
in the mode of derivation and accumulation of the materials com-
posing the sedimentary series of the northern and southern groups,
P
200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
as well as their zoological differences, are matter for much research.
Materials have not long been obtained whereby we may institute
comparisons between the different members even of the British
group of Carboniferous rocks, setting aside our intimate connexion
on the one hand with the European, and on the other with that of
the American continent, especially New Brunswick and Nova Scotia,
whose relation to Scotland through the Coal-measures can
hardly be doubted. Those beds which overlie the Carboniferous
Limestone in the south of Ireland have hardly yet had assigned
to them their true place by correlation with those of England;
neither has it been satisfactorily settled what is the precise strati-
graphical commencement of the Lower Carboniferous series of the
North-Devon area, or where the line should be drawn between the
Upper Devonian and Lower Carboniferous. Both horizons are
fossiliferous, and it is only in the south of Ireland that we have
similar conditions, or where a comparison can be instituted be-
tween the two. Again, as regards the Coal-measure “shales and
flags ” immediately overlying the Carboniferous Limestones of the
south of Ireland, there can be no doubt that they represent the
Millstone Grit of the English Coal-fields. This was the opinion of
the late Professor Jukes, who, in the explanatory memoir to sheet
No. 137 of the Irish Geological Survey maps, says, ‘‘ Doubtless the
whole of the Coal-measure series of Central Ireland is contempo-
raneous with the lower part only of that of Central England, in-
cluding the Millstone Grit in that lower part.” Prof. Hull also
doubts not that through the identification of the Gannister beds in
the Leinster Coal-field, which, in the north of England, overlie
the Millstone Grit, that contemporaneity, to a large extent, occurs
between the English and Irish Carboniferous beds, and this especially
on physical grounds.
Through the close research of the Irish Survey in the Leinster
and Munster Coal-fields they are now enabled to trace out and
distinguish four divisions:—1, the Yoredale beds; 2, the Millstone
Grit ; 3, the Gannister beds; and 4, the Middle Coal-measures as
determined in England. Hitherto they have simply been classed
under the general term ‘‘ Coal-measures.’’
Professor Hull endeavours to show to what extent the British
Carboniferous rocks have their representatives in Ireland; and he
also proposes to establish a ‘‘ Middle Carboniferous series,’ which
shall include all the strata lying between the Carboniferous Lime-
stone and the Middle Coal-measures, including the Yoredale beds,
Millstone Grit, and Gannister beds. Mr. Hull is careful to impress
upon us the fact that the Yoredale beds of Ireland are more inti-
mately associated with the Millstone Grit and Gannister beds than
with the Carboniferous Limestone; hence his reason for proposing
the new classification. In England the Yoredale beds are most
closely allied to the Carboniferous Limestone, upon which they con-
formably rest.
Mr. Hull minutely describes the main features of the Southern
and Northern Irish Coal-districts and their subordinate Coal-fields.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 201
In the southern coal-fields of Carlow, Queen’s County, Kilkenny, &c.
the succession of the strata above the Carboniferous Limestone is
remarkably uniform and constant; any one may be taken as the
type of the whole, having reference to an English standard for
comparison *,
The Northern Coal-district in Ireland includes the Leitrim and
Tyrone Coal-fields, which are representative of the southern in all
their successive beds and stages. Isolated geologically occurs the
Ballycastle Coal-field of Co, Antrim, the Irish representative of the
Clyde Coal-basin, of Lower Carboniferous age, a conclusion estab-
lished and confirmed through its fauna. The Carboniferous Lime-
stone here is only a few feet in thickness, its place being taken by
sedimentary or mechanical deposits. This is paralleled in North
Britain ; but the same beds thicken to the south-west in Derbyshire
and attain a thickness of 5000 feet of solid limestone.
The English and Scotch Carboniferous districts and their respective
coal-fields receive from Prof. Hull terse but careful analysis in his
paper, each coal-field being divided into recognized stages varying
from A—G, or from the Calciferous Sandstone series of the Scottish
beds (A) to the Upper Coal-measures of any coal-field (G).
I deem it important for my analysis of the Carboniferous system
to state concisely the subdivisions or stages into which they are
divided. I adopt the classification clearly given by Professor Hull,
which is mainly that of the English, Scotch, and Irish surveys. I
omit the physical characters of the beds, reference to his paper being
better +.
The British Carboniferous Series in descending order, with
localities.
Names of Formations. Localities.
(Stage G. Upper Coal-measures. Manchester, Stoke-on-Trent,
Thin coal-seams and lime- Newcastle-under-Lyne, 5S.
| stones. part of Dudley Coal-field ;
Fossils (freshwater or ma- banks of the Dee near
i rine): Fish; Crustacea, Ruabon; Hamilton and
Essentially | Cythere inflata; Annelida, Ayrshire, Scotland.
Freshwater | Spirorbis carbonarius.
and Stage EF. Middle Coal-mea- Central portions of all the coal-
Estuarine 4 sures. 'Thick coals. fieldsof England and Wales ;
Beds. Fossils (freshwater or es- Upper Ooal-measures of
tuarine): Fish ; Mollusca, Scotland.
Anthracosia, Anthraco-
mya; Crustacea, Beyri-
chia, Estheria; Annelida,
Spirorbis. Marine species
rare,
alco
* Prof. Hull describes the Castlecomer and Killenaule Coal-fields. Vide
explanations of Sheets 136 and 137 of maps of the Geological Survey of Ireland ;
also the Slieveardagh Coal-field, Co. Tipperary.
t Quart. Journ. Geol. Soc. vol. xxxiii. pp. 613-616.
202
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
British Carboniferous Series §¢. (continued).
Names of Formations.
( Stage E. Gannister Beds, or
Lower Coal-measures.
Thin coals with hard sili-
ceous floors; flagstones
and shales.
| Fossils (marine): Fish (mi-
gratory); Mollusca, Goni-
atites, Discites, Orthoceras,
Posidonomya,Monotis, Ari-
culopecten, Anthracosia,
Lingula, &e.
Stage D. Millstone- Grit Series.
Coarse grits, flagstones,
and shales, a few thin
coal-seams.
Fossils: similar to those
of the Lower Coal-mea-
sures.
Stage C. Yoredale Series.
Shales and grits, passing
down into dark shales
and earthy limestones.
Fossils (marine): including
Goniatites, Aviculopecten,
Ctenodonta, Chonetes,
Discina, Posidonomya,
Productus, &e.
(Stage B. Carboniferous Lime-
stone. Massive limestone
in many beds with inter-
vening shales and grits
(thick in the south, thin
in the north).
Fossils: Fish, Crustacea,
Crinoids, Corals, &e.; all
marine.
Stage A. Lower Limestone
Shale and Calciferous
Sandstone. Dark shales
| in some places; grits,
conglomerates, and red
| sandstone and shales in
the northern districts.
| Fossils (marine).
Basis. Upper Old Red Sand-
stone. Yellow sandstones
and conglomerates.
Fossils (freshwater): not
well represented in Eng-
land.
Essentially y
Marine.
OOO
Kssentially |
Marine |
(except
Stage A 4
in
Scotland).
Localities.
South Lancashire, North Staf-
fordshire, Nurth and South
Wales.
Uplands of Yorkshire, Lanca-
shire, and Derbyshire, N.
Staffordshire, and N. and
S. Wales.
Uplands and valleys of Lanca-
shire, Yorkshire, Derby-
shire, North Staffordshire,
Wales, &e.
North and South Wales, Derby-
shire, Yorkshire, Cumber-
land; in Scotland the
Lower or Main Limestone.
South Wales, Gloucestershire
and Somersetshire, Nor-
thumberland and Durham ;
in Scotland, Calciterous
Sandstone series.
South Wales, Northumberland,
Scotland (Dura Den), Ire-
land (Kiltorcan).
The above stages contain, in all, about 500 genera and 2400
species.
I purpose showing their numerical value and relation one
to the other in the passage of the species through the 8 horizons
or stages to the close of the Carboniferous period. The connexion
of the Permian rocks with the Carboniferous is not an easy task,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 203
small as the fauna is known to be; but I-shall reserve this as the
basis of my next address, if permitted to do so.
The recent work of the Geological Survey has proved that the
greater part of the Calciferous Sandstone of Scotland is the equivalent
in time of the.true Carboniferous Limestone of England. Most of
the Carboniferous Limestone of Scotland is the equivalent in time
of the Yoredale rocks of Yorkshire; so also is most of that
part of the Carboniferous Limestone series of Northumberland
from which lists of fossils have been published. In fact the terms
Calciferous Sandstone, Lower Limestone Shales, Carboniferous
Limestone, and Yoredale Rocks must really be regarded as repre-
senting conditions of depth and deposit, and not, when comparing
different areas, as representing relative age. I have had great
difficulty in dealing with the Yoredale species, as well as those
from the Lower Limestone Shales, arising from the terms ‘‘ Lower
Limestone” of the north of England and Scotland and Lower
Limestone Shale of the South-west of England and South Wales not
being always applied to the same horizons by different authors.
Physically in South Wales, Gloucestershire, and Somersetshire they
can be definitely traced and mapped, carrying with them an unmis-
takable suite of fossils, differing essentially from the Great, or Scaur,
or Carboniferous Limestone above; entirely destitute of many
zoological groups, especially the compound Actinozoa, the Bryozoa,
and the Cephalopoda; abounding in fish-remains, chiefly Placoidei
(teeth and spines).
The comparison of the Northumberland, Durham, Yorkshire, -
and Lancashire rocks amongst themselves, and further correlation
with the Scotch series, has yet to be effected; but the three groups
in the table at p. 226 (viz. the Lower Limestone shales, the Carbo-
niferous Limestone, and the Yoredale rocks) present, as nearly as
possible, the census of species as now received and recorded.
In the Pendle and Clitheroe area the Yoredale rocks are of great
thickness, 3000-4000 feet ; they are scarcely represented in Scotland,
although so near; whilst the great or ‘“‘ Scaur-limestone” of Derby-
shire is represented in Northumberland. The probable arrangement
and agreement of the North-of-England and Central-Scottish stages
have been arranged or correlated by Mr. Hull, through a tacit
agreement with Professor Geikie and Mr. Lebour, both on strati-
graphical and paleontological grounds. The stages are as follows :—
North of England. Central Scotland.
Stages HE. Gannister beds. EK. Slaty-black-band series.
D. Millstone Grit. D. Moorstone-rock series.
“Great Limestone.” Upper Limestone series.
C C (Yoredale beds.)
’ | Flagstone and Shales. * ) Lower Coal-and-Ironstone
series.
B. “ Scaur-Limestone series.” B. Lower Limestone series.
Sometimes absent. ; t :
A. { («“ Tuedian.”) \ A. Calciferous Sandstone series.
Mr. Lebour, in corroboration of this, compared lists of fossils from
the “ Great Limestone” of Northumberland (‘‘the most marked
204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Yoredale bed”) with the prepared Scotch list, and found that 32
species Were not known in Scotland, and that about 60 species ran
through or were common to the three Scotch divisions, and also
that 28 were found in the Scotch upper and middle series only, 10
being found only in the lower series. This community of 28 species
corroborates Mr. Hull’s views, who believes that geographical posi-
tion, through an interposed Silurian barrier, separated the Scotch
and English marine areas. ‘There can be no doubt also that over
the whole of the north of England and the borderland of Scotland
shallow-sea, estuarine, and land conditions largely prevailed during
the earlier, if not the middle, Carboniferous stages. It is by such
conditions that correlation is rendered difficult over extended areas;
and only by patient, long-continued work with a definite end or pur-
pose, changes both on the dip and strike being carefully mapped
or recorded, can the subdivision of one region be actually compared
with that of another. IJtis from this want of uniformity in working
that various horizons are adopted for the same beds by different
authors, and that ranges of fossils are made to differ also. A very
important table is appended to Mr. Hull’s paper, giving the census
or known fauna and vertical range of the marine genera and species
of the Gannister beds (stage E). All these species are embodied in
the numerical estimate in my own table. 36 genera and 69 species
are enumerated by Mr. Baily; all the genera and 40 species ascend
upwards or come from the underlying Carboniferous Limestone.
Mr. Baily determines that only 6 species of the 69 pass to Stages F
and G. They are Goniatites Listerr, G. Looneyt, Conularia quadri-
sulcata, Aviculopecten papyraceus, Discna nitida, and Productus
scabriculus. No marine shells occur in the Upper Coal-measures in
the table, Spirorbis carbonarius and Anthracosia only characterizing
the Stage G. Baily also states that 18 species are peculiar to Stage
E, or the Gannister beds *.
Professor Hull in his paper gives a table of the “ Continental
equivalents of the British Carboniferous divisions,” and a table also
of ‘‘ Representative Carboniferous formations,” both of great use in
classification. A fourth table is added, showing the vertical range
of the marine genera and species of Stage F (Middle Coal-measures).
Prant#.—Large as the Devonian flora of America appears to
have been, it bears no comparison with the succeeding Carboniferous
group, either in America, Britain, or HKurope. 95 genera and
about 320 species constitute the whole of the known Devonian
Plante, through the universality of their distribution. That much
of the Carboniferous flora was derived from the Devonian is evident.
Of the 84 British Carboniferous genera, 36 occurred in the De-
vonian, and these are also the most typical or marked in the
Carboniferous system.
We owe our chief knowledge of the Devonian and Carboniferous
flora of North America to Dr. Dawson, of Montreal, Vanuxem,
Hartt, Rogers, Lesquereux, Newberry, and others, who have largely
added to the literature of the fossil flora of the American Continent.
* Quart. Journ. Geol. Soc. vol. xxxiii. pp. 613-651.
ANNIVERSARY ADDRESS OF THE PRESIDENT, 205
The British Devonian flora is small, including only 12 genera and
18 species, as stated in the Devonian table. The American
genera and species of the Carboniferons flora number, according to the
published lists &c., 94 genera and 695 species; and the European
Carboniferous flora, including the British, 176 genera and 1370
species ; the species occurring in the 8 divisions of our Carboniferous
strata number 339, illustrating 84 genera. The stratigraphical
distribution is as follows :—
Calciferous Sandstone ...... 10 genera and 12 species.
Lower Limestone Shale .... 22 ze 44,
Carboniferous Limestone.... 13 Se DAY nce
Moredale Rocks ......... HONEY p55 none ,,
Malistone Grit: is... ce 3 6 ws 10 = 254s
Lower Coal-measures ...... 54 ss A i lege Ps
Middle stele. (uteri bn hide 34 = 1
Upper ce i eee ee 33 a 168 Fx.
Ten genera are largely represented in Britain, and contain 192
species out of the 339, forming the whole flora: they are Alethopteris
9 species, Asterophyllites 11, Calamites 14, Lepidodendron 21, Lepido-
strobus 15 (but for the number given, these cones of Lepidodendron
should be taken as that genus ; probably we may never know to what
species of Lepidodendron all these Lepidostrobi belong), Neuropteris
23, Pecopteris 28, Szgillaria 27, Sphenopteris 32, Ulodendron 12. All
the Alethopterides are from the Coal-measures. The Asterophyllites,
with two exceptions (A. foliosus and A. longifolia), are also Coal-
measure fossils. The Calamites range from the Calciferous Sandstone
to the Upper Coal-measures—4 species, C. canneformis, Schloth.,
C. cultranensis, Haught., C. dubius, Artis, and C. Lindleyz, Sternb.,
occurring in and below the Carboniferous Limestone; the remaining
10 are Coal-measure forms and mostly belong to the Lower series.
The 21 species of Lepidodendron, with 5 exceptions, are all from
the Coal-measures, as are 13 of the 15 Lepidostrobi; 2 species
(L. comosus, L. & H., and L. variabilis, L. & H.) are Lower Limestone
Shale species. With one exception in the genus Newropteris (NV.
Toshi), the species are from the Coal-measures ; although we know
that NV. cordata, N. flexuosa, and NV. gigantea are Millstone-Grit
forms. No Pecopteris is known below the Lower Coal-measures ;
therefore the large number of species (28) are essentially Upper
Carboniterous. Of the 27 species of Szgillarza only 2 occur below the
Lower Coal-measures, viz. S. dichotoma, Haught., and S. pachyderma,
Brongn., which occur in the shales at the base of the Carboniferous
limestone. 3 species of Sphenopteris (S. affinis, S. linearis, and S. tri-
foliata) range from the Calciferous Sandstone to the Coal-measures ;
4A others (S. bifida, L. & H., S. crassa, L. & H., S. elegans, Brongn.,
and S. obovata) occur in the Carboniferous shale and limestone;
the remaining 25 species irregularly range through the Lower,
Middle, and Upper Coal-measures. Ulodendron minus and U. par-
matum range from the Carboniferous shale to the Upper Coal-
206 PROCEEDINGS CF THE GEOLOGICAL SOCIETY.
measures. U. Landleyanum, U. majus, and U. minus are the Mill-
stone-Grit species. The above 10 genera were selected on account
of their being largely represented specifically. Regarding the
distribution of the Carboniferous flora, we know that many species
occurring in Pennsylvania and Nova Scotia are identical with Euro-
pean and British species. This points to a greater similarity and
equality of climate than now prevails, and also to the possible con-
nexion of the coal-hearing areas of Europe with that of America,
either by continuous land or by groups of islands.
It is difficult in all cases to determine from the often somewhat
vague descriptions of authors the true geological horizon of the
many species in the true Coal-measures, or whether they are
Upper, Middle, or Lower Coal-measure forms. Every care, however,
has been taken to determine this when possible, not only for the
Plantee but for the whole fauna also.
Protozoa: SponerpaA.—The 10. genera and 15 species known
are confined to the Carboniferous Limestone and shales below.
The genus Paleacis of Haime (1860) now embraces Phillips’s,
Hydriopora, M‘Coy’s Astreopora, Seebach’s Paleacis, and the genus
Sphenopoterium of Meek and Worthen. ‘The 3 British species,
P. cuneiform, J. Haime, P. cyclostoma, Phill., and P. obtusa, Meek
and Worthen, have a wide geographical range, being almost uni-
versally distributed ; but none of the 10 genera and 15 species have
occurred above the Carboniferous Limestone in any area.
Protozoa: FoRAMINIFERA.—14 genera (11 belonging to the Im-
perforata and 3 to the Perforata), with 48 species, range through the
lower portion of the Carboniferous group, but none have yet occurred
higher than the Yoredale rocks, where 7 genera and 18 species are
. found, and only 1 genus (Stacheia) is known in the Calciferous
Sandstone ; 6 species illustrate Stacheia, and all range from the Cal-
ciferous beds to the Carboniferous Limestone. Our knowledge of
this order (Reticularia) of the Rhizopoda in the Carboniferous rocks is
due to the labours and researches of Mr. H. B. Brady. 40 species are
known from the Carboniferous Limestone. 43 of the 48 species in
these rocks are named and described by Mr. Brady in his learned
monograph upon the British Carboniferous and Permian Fora-
minifera in the volume of the Paleontographical Society for 1876.
Hyprozoa.—Arbusculites and Palwocoryne are the only 2 known
genera in this class. <Arbusculites argenteus, with Palwocoryne
radiata and P. scotica (all three from the Carboniferous Limestone),
complete the list.
ActinozoA.—Both the Tabulata and Rugosa are well repre-
sented in the Carboniferous rocks, especially the Rugosa. 21
genera fall under that order, and 14 in that of the Tabulata.
The genus Cladochonus of M‘Coy (Jania of the same author) and
Aulopora are the only representatives of the Tubulosa. Aulopora,
which is probably the young state of Syringopora, usually referred
to the Tubulosa, must be placed with the Tabulata if so deter-
mined. 9 families, 36 genera, and 141 species constitute the
Actinozoal fauna. The only 2 families of numerical value are the
ANNIVERSARY ADDRESS OF THE PRESIDENT. 207
Favositide, with 5 genera, and Cyathophyllide, with 20; the
remaining 7 families have only 1 or 2 genera each and but few species.
No form of Coral is known above the Yoredale rocks, and only
2 genera and 2 species occur in the Yoredale series, viz. Mavosites
tumidus, Phill., and Zaphrentis Phillipsu, M.-Edw. The Calciferous
Sandstones yield 3 species, Alveolites septosus, Fleming, Mavosites
tumidus, Phill., and Lithostrotion junceum, Fleming.
The Lower Limestone Shales (mostly those of the west of England)
have yielded 13 genera and 30 species; the nature of the deposit
greatly influenced and determined the presence of the species.
Nearly all the Corals in the shales are simple forms and dwarfed
in habit, certainly more so than those species that lived in
clearer and deeper water, where lived most of the compound
forms which occur so abundantly in the limestone beds. This
difference, under petrological association, is manifest on carefully
examining the stratigraphical position of the corals in many locali-
ties. The Carboniferous Limestone is coralliferous throughout,
and the fullest evidence may be obtained of large and extensive
reefs composed essentially or mainly of the Rugosa, Lithostrotion,
Lonsdaleia, species of Cyathophyllum, and numerous other species.
The Carboniferous Limestone of the British Islands yields every
known genus and species catalogued; in other words, 36 genera
and 141 species (all the Carboniferous Actinozoa known) are found
in the Carboniferous Limestone in one locality or other in Great
Britain and Ireland. The whole class culminates in the Mountain
Limestone, for only 2 genera and 2 species pass to the Yoredale beds
(favosites tumidus and Zaphrentis Phillipsu). This sudden ter-
mination in time of the Actinozoa was undoubtedly due to those
physical changes which took place in consequence of the elevation of
the sea-bed and prior to the deposition of the Permian. Our lists,
tables, and collections of the Carboniferous Corals have not been
studied sufficiently to enable us to construct proper distribution
tables ; but the accompanying table of 19 of the chief British genera
is intended to show their geographical distribution in Britain, also
in the chief locality in Europe, and further their correlation with
America.
208 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Table showing the numerical value of the species in the chief genera
of Actinozoa in Great Britain, Belgium, and America, the
former for European, the latter for American comparison.
{D)
©
tg = : ; 3 5
eH el |=
eS le | ee ae
el ee gia | aes
Amiplexusien ees daoe teaetececlerads 6 “ 4 12 9) 21
JMO) Nay AblTIO Goo sscnasqaceanosadoc 2 2 2 wae ie 6
@hestetesy vssyemeecscatceercs sence 4 2 4 2 3 15
Cladochonuseaereercan cect 4 a 2 2 Ms 8
Clisnoyolaylknwan » .sssoondacodosdaoose 4 5 4 3 O0 16
Cyathaxomlanecoseuosncasccrea es 2 1 a 3 6 12
Cyathoplayllunayeeasceeseee ea ilo 5 6 7 3 32
Cycloplivlllmmam ena cence 2 2 1 235 ee 5
I AVOSICES Ie lacersus as seleciene a match: 6 i 3 5 3 18
leterop nwvilliaige cee reece a eee 2 6 ss shee ee 8
JUNI NOSHROELO sonsccosnaeccoossn0s 16 10 12 4 5 47
Thonsdaleran ii wissen nese 4 2 ay 1 1 8
Miche liniajaeeepeeccseeeee tate 4 2 5 4 1 16
Pallgeacisth veces asus coctetlestane 1 2 ae 2 ~cieie tite
ehilllijpsastreca ycpemencdee csc: 2 cS. ie Hf Bee 2
SH ABUTYERO) COTES) BGs anasaeodoodsqunanesqs 5 3 6 5 4 23
ZL PATemuis ie se acces sce eneesce es 8 10 5 21 18 62
83 57 54 al 49 | 304
Ecuinoprrmata.—tThe class Echinodermata is represented in the
Carboniferous rocks by 4 orders—the Crinoidea, the Blastoidea, the
Perischoechinoidea, and the Echinoidea. The Holothuroidea through
the Synaptz occur also in a few localities. 30 genera and 163
species constitute the entire fauna, and the whole are in the Car-
boniferous Limestone division. Only 1 species (Archeocidaris Uret)
seems to be known in the Calciferous Sandstone. No species
appears in the Yoredale rocks; indeed the entire class ceases to
appear above the Carboniferous Limestone, the 5 succeeding
divisions being utterly void of this class and the Coelenterata. The
Lower Limestone Shales through 11 genera yield 31 species—Actino-
crinus 5, Archeocidaris 3, Astrocrinus 1, Atocrinus 1, Cyathocrinus 2,
Palechinus 3, Platycrinus 10, Poteriocrinus 3, Rhodocrinus 2, and
Taxocrinus 1 species. Only 1 of the above is special or confined
to the Lower Carboniferous Limestone of Carlops, Peeblesshire,
Astrocrimtes (Zygocrinus) Benner, R. Ether., jun.
The characteristic genera, and those containing the largest
number of species, are :—Actinocrinus 21 species, 5 of the 21 occur-
ring in the Lower Limestone Shale ; Cyathocrinus 10 species, 2 of
the 10 are also Lower Limestone Shale; Platycrinus 25 species,
10 of which are in the Lower Limestone Shale ; /hodocrinus 12
species; and <Archwocidaris 10 species, The order Blastoidea,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 209
through the Pentremitide, 16 species, and Pentaphyllum 1 species,
are all confined to the Carboniferous Limestone proper. The sin-
gular group of the Perischoechinoidea, with Palwchinus 7 species,
Perischodomus and Melonites 1 each, also essentially characterize the
Carboniferous Limestone proper.
ANNELIDA.—4 species of this class, belonging to 13 genera, wander
through the 8 divisions. Spzrorbis numbers 14 species and Serpula 6;
the remaining 11 genera have only 1 or 2 species each. Serpulites
carbonarius, Spirorbis pusillus, S. caperatus, and S. helicteres are the
only 4 species that range above the Carboniferous Limestone and into
the Coal-measures where the argillaceous shales and clays are of
marine or estuarine origin. The Calciferous Sandstones of Scot-
land, through the researches of Bennie, have yielded Serpulites
carbonarius, Spirorbis Kichwaldi,S. globosus, S. helicteres, S. pusillus,
and 2 varieties. 16 species occur in the Lower Limestone Shale ;
10 genera and 24 species in the Carboniferous Limestone. Serpulites
membranaceus is the only Yoredale form ; and 4 species, Crossopodia
Embletone, C. media, Serpulites carbonarius, and Spirorbis pusillus,
occur in the Millstone Grit ; and Serpulites carbonarius is the only
Lower Coal-measure form, also associated with Arenicola carbonaria.
The same 2 species are Middle and Upper Coal-measures, which
exhausts the Annelidan fauna.
Crustacua.—The remarkable Crustacean fauna that occurs in the
Silurian rocks numbers about 320 species, chiefly Trilobites, all of
which, with the exception of 5 or 6 genera, died out entirely at the
close of the Silurian period. The Crustacea of the Old Red Sandstone
belong chiefly to the order Merostomata—Hurypterus, Pterygotus, and
Stylonurus being the characteristic genera. The Trilobita, comprising
only 6 genera (Bronteus, Cheirurus, Harpes, Homalonotus, Phacops,
and Phillipsia), with 11 species, are Devonian, no Trilobite occurring
in the Old Red proper. The Carboniferous system in Britain yields
35 genera and 225 species, 130 of which are Ostracoda, 59 Phyllopoda,
2 Merostomata, 6 Pcecilopoda, 2 Stomapoda, 5 Macrura, and 13 Tri-
lobita, illustrating the 3 genera, Brachymetopus (2), Griffithides (5),
and Phillipsia (6), which group entirely disappears with the close
of the Carboniferous Limestone. Nowhere in Europe or America
have we evidence of the continuity of this group above the rocks
named. Beyond the Ostracoda and Phyllopoda, which constitute
the 2 important orders in the Carboniferous rocks (together num-
bering 189 species out of the 225 known), there is little to discuss.
The genera of Ostracoda number 85, the Phyllopoda 8, the Trilobita
only 3.
The CatcrrErovs Sanpstone (Tuedian) has yielded 9 genera and
20 species, mostly Ostracoda, and 2 species of Anthrapalemon, the
first known appearance of the group or tribe Macrura. (38 other
species of the same genus occur in the Coal-measures.)
Lower Limxstonn Suates.—17 genera and 48 species, also chiefly
Ostracoda and Phyllopoda, are individually abundant in the Lower
Carboniferous beds (below the Carboniferous Limestone).
CaRBONIFEROUS LimEstoNE.—159 species are recognized and de-
210 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
scribed from the Carboniferous Limestone proper, illustrating 28
genera out of 33 (or nearly every occurring genus is represented),
and the above number of species out of the known 225. The
4 genera wanting in the Limestone are Anthrapalemon, Belinurus,
Pygocephalus, and Candona. The Ostracoda number no less than
15 genera and 107 species; the Phyllopoda 8 genera and 36
species ; the Trilobita 3 genera and 8 species.
YorEDALE Brps.—The Ostracoda through the genus Bairdia
(6 species) and Kirkbya (2); the Phyllopoda through Beyrichia (5),
Estheria (1); and Griffithides mucronatus (Trilobita), complete the
Crustacean fauna of this horizon.
Mittsrone Grir.—No Crustacean remains known.
Lower CoaL-mMEasuRes.—13 species of Ostracoda, 8 of Phyllopoda,
and 4 Peecilopoda, with 3 species of the genus Anthrapalemon, a
Macrurous Decapod, 2 species of which first appeared in the
Calciferous Sandstone (A. Maconochii, Ether., and A. Wood-
wardi, Ether.). A. dubius, Prestw., A. Grossarti, Salt., and A. Rus-
sellianus, Salt., belong to the Lower and Upper Coal-measures. This
is the earliest known appearance of the order Decapoda. This ancient
type has been found both in the Coal-measures of Europe and
North America. Anthrapalemon is related to the living Galathea.
Of the suborder Xiphosura or Pecilopoda we possess 2 genera,
Bellinurus and Prestwichia, this last allied to Neolimulus of the
Upper Silurian. The Penny-stones of Coalbrook Dale yield Prest-
wichia rotundata (Limulus). All the thoracic and abdominal seg-
ments in Prestwichia are ankylosed. The earliest appearance in
time or commencement of existence of the Xiphosura is in the
Ludlow rocks; no Xiphosuran has yet been detected in the Deyo-
nian. Pygocephalus Cooperi, Huxl., and P. Huxley, Woodw., occur
in the Lower Coal-measures. These Podophthalmatous Stomapods,
with the Decapod Anthrapalemon (3 species), carry back in time
the higher order of the Crustacea.
MippLe Coan-mEAsvrEs.—Anthrapalemon dubwus, Bellinurus bel-
lulus, Konig, Beyrichia arcuata and B. Binneyana, Hstheria Bei-
nertiana and H. striata, are all the Crustacea known in the Middle
Coal-measures.
Upper Coat-mMrasvrEs.—10 genera and 16 species compose the
Crustacean fauna of the Upper Coal-measures—Ostracoda 6, Phyllo-
poda 7, Poecilopoda 1, and Anthrapalemon Grossariv.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 211
Number of Species in the six Paleozoic orders of the Crustacea
occurring in England, Scotland, and Ireland; also in Belgium
and America. ‘The two latter areas for comparison as betore.
cs} se i FS
| q oS =| Ss
Orders. a = 2 5 o
cold) |
S @ oO S
ey oD) = aa <
SRI OMG ta acacs afelscecawicae odes ead 45 68 38 21 9
HSPN O POCA) acs. ctdenra coe ecscess: Ils} = 48) 14 9 11
PREMMOSUMA Fi t)44 class seadeeceeessee ees 8 1 5) Bs 2
Bina AbOTIG A! 4). 5.0550. 0cs- accesses eae 1 2 che se Ze
Ble GAMOU A) cp ton sae cease sinc sobiesnias 1 7
Tsong eee ee ee 18 7 14 15 26
ae g5 |il4 | 71 | 45 | 50
Bryozoa.—The Carboniferous Bryozoa as a group constitute by far
the largest series in any division of the Paleeozoic rocks. 77 species
range through the 3 lower horizons of the Carboniferous series, 74
belonging to the true Carboniferous Limestone, 28 to the Lower Lime-
stone Shales or Lower Limestones, and 4 to the Calciferous series ; not
a single species passes to or occurs in the Yoredale, Millstone Grit, or
either one of the three divisions of the Coal-measures. The whole
group essentially belongs to and characterizes the Calcareous rocks
and shales at the base of the formation; the large genera are—
Ceriopora 5 species, Fenestella 26, Glauconome (Acanthocladia) 8, and
Polypora 8. 20 other genera of great zoological value occur, but the
species are few in each genus(1 to 4). Actinostoma, Carinella, Dras-
topora, Gomoclacia, Hemitrypa, Ptilopora, Rhabdomeson, Synocladia,
and Vineularia are important genera in the Carboniferous rocks,
and distinctively determine the age of the beds in which they occur.
Be it remembered that none of the Paleozoic genera live on or
extend into the Mesozoic period, and the Fenestellide become
extinet in the Permian rocks. 24 genera and 77 species at present
represent the fauna of this division of the Molluscoida; doubtless
the species will be much reduced through extended research and
eritical examination*; but as Mr. Shrubsole is carrying on research
in the Fenestellide, and Mr. Vine investigating the Diastoporide, it
is better to give the census of the species as they now stand without
incomplete modification. Mr. Shrubsole’s last paper is not yet pub-
lished; I will therefore notice their distribution, subject to the
anticipated work of these two authors.
CaLCIFEROUS SANDSTONE.—Archeopora nexilrs, Cerropora similis,
Fenestella Morrisui, F. plebera, F. tuberculato-carinata, and Glauco-
* Vide the able papers by Mr. Shrubsole, F.G.S., and Mr. G. R. Vine in the
‘Quarterly Journal of the Geological Society,’ vel. xxxvi.; also Vine, ‘ Report of
the British Association,’ 1880, “On the Carboniferous Polyzoa,” for important
matter relative to the history and classification of the Polyzoa.
212 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
nome gracilis appear to be all known in these lowest beds of the
northern Carboniferous rocks.
Lower LimestonE AND SHALES.—13 genera and 26 species illustrate
these shaly limestones at the base of the Carboniferous; the 3
chief genera are—Venestella 12 species (far too numerous), Glau-
conome 3, and Pustulipora 2 species; the remaining 9 genera have
only 1 species each; many of these, necessarily, also occur in the
succeeding Carboniferous Limestone.
CsRBoniFEROUSs LimEstonE.—72 species occur, belonging to 19
genera; the most important of the latter are—Fenestella with
25 species, Glauconome 8, Polypora 8, Rhabdomeson 3, Pustulipora
4, and Cercopora 5 species. The 13 remaining genera, although
poor in species, are highly characteristic; amongst them may be
named Sulcoretepora, Synocladia, Vincularia, Actinostoma, and Dias-
topora. No species passes to higher strata or above the Carboni-
ferous Limestone.
ARACHNIDA.—Only in the Lower Coal-measures have we detected
the Arachnida, 5 species representing 3 genera—Architarbus sub-
ovalis, H. Woodw., Hophrynus Prestvicit, Busk, Hoscorpius anglicus,
H. Woodw., and &. carbonarius, Meek and Worth.; an unde-
scribed form occurs, which, however, may be H.anglicus. E. carbo-
narius 1s also an American species, occurring in the Coal-measures
of Illinois; and Architarbus is also a North-American form. The
occurrence of two of the three genera and one species in two
areas so widely separated is significant, with many other facts, of
the probability of the continuity of land between Britain and
America during the long period required for the deposition of the
Coal-measures and the accumulation of coal.
Myrropopa.—The 2 genera of Chilognathous Myriopoda, Hupho-
beria and Xylobius, which occur in our Coal-measures are also
American, and, with the Arachnida, again add strong presump-
tion to land-continuity, densely covered with that peculiar flora
known to have flourished during the Coal-measure period. We
possess 3 species of Huphoberia, viz. HL. anthrax, Salt., LE. Brownia,
H. Woodw., and £. ferov, Salt. Dr. Dawson’s genus Xylobius, also
the known American species ‘“ Stgillarue,” lends additional interest
to the attempt to correlate our fauna and flora of the Coal-measures
with those of the American continent; for many species of plants
are identical, and with them associated faunal groups.
Insecra.—Both the Orthoptera and Coleoptera are represented in
our Coal-measures. The Mantide through the genus /ithomantis
of Dr. H. Woodward, the Locustide through Giryllacris, Swinton ;
these two genera belong to the Orthoptera. The genus Curculiordes
of Dr. Buckland belongs to the Coleoptera. These all occur in our
Lower Coal-measures. Their history and zoological affinities have
been ably described by Dr. H. Woodward, F.R.S., in the ‘ Journal ’
of our Society (vol. xxxii.); doubtless every fresh investigation into
the rocks that hold and yield the extinct flora of our coal-fields will
bring to light the remains of the three last groups, the Arachnida,
Myriopoda, and Insecta; they are, or were, intimately associated
ANNIVERSARY ADDRESS OF THE PRESIDENT. 213
with the vegetation of the Carboniferous epoch, and, with other
remains in the same rocks, show that the Atlantic ocean covers a
vast area of once continuous or contiguous land.
Eyery one who has studied the varied conditions of the Carbo-
niferous series, the deposition of its strata, the distribution of its
fauna, will at once admit that its history is only to be written
through the great and reliable group of the Mollusca (Brachiopoda,
Lamellibranchiata, Gasteropoda, Pteropoda, Heteropoda, and Cepha-
lopoda), whose 6 divisions or classes number 116 genera and 1020
species, or nearly one half the entire known Carboniferous fauna. So
many of the genera have come down to the present day, that infe-
entially, through observation, we know their habits in Carboniferous
times; they show us that, during or throughout the accumulation
of the Carboniferous Limestone, moderately deep-sea conditions
prevailed, and the Molluscan fauna then surpassed all subsequent
numerical development during the Carboniferous period. Ultimately
physical changes caused the sea to shallow, thus altering all bathy-
metrical conditions at the same time: littoral species died out,
through altered circumstances; and the habits of the deeper-sea
fauna changed also on slow elevation, the zonal lines of life under-
going modification through adaptation. Plainly are these modifi-
cations and changes to be observed through the several stages, from
the Calciferous Sandstones to the summit of the Coal-measures.
Zoologically, only the last five stages of the Carboniferous group
have to be considered, as so great a change took place at the close of
the Gannister group or Lower Coal-measures, the succeeding beds
illustrating terrestrial conditions through the rich and earliest exten-
sive flora known (vide Table at end of Carboniferous system, p. 226).
No one has felt the difficulty of showing the distribution of life
through the Carboniferous group more than myself, the rich fauna
that characterizes the series from the Calciferous Sandstones to the
top of the Gannister (or Lower Coal-measure) beds being most diffi-
cult of analysis.
Every extended sea-bed has its own conditions and its own fauna;
the exact nature of that sea-bottom it is difficult to predicate; it
can only be learnt through examination. Admitting that the fauna
of any group of rocks is, or was, as local as the physical condi-
tions during deposition, and the maximum of life is usually local,
it will show itself in any area, in any part of an epoch or of a
stage; it is governed chiefly by the nature of the sediment and
by temperature. The questions of appearance of species, duration,
migration, extinction, recurrence, and many other conditions that
govern marine life in all its phases are to be studied through a
careful investigation of the physical history of the Carboniferous
rocks ; and through no other zoological group do we receive so much
instruction as through the Mollusca.
Bracuropopa.—Both the Tretenterata, or “‘ Inarticulata,”’ and the
Clistenterata, or “ Articulata,” are largely represented in the Carbo-
niferous rocks; and many genera appear for the first time, and
VOL. XXXYVII. gq
214 PROCEEDINGS OF THE GROLOGICAL SOCIETY.
essentially characterize the lower members of the Carboniferous
group: such are Hypodema and Syringothyris, neither of these
appearing in older strata.
The specific development of Productus has no precedent or parallel
in any other group of British strata. 44 species occur in the deposits
from the Calciforous Sandstone to the Lower Coal-measures, 5 species
in the Calciferous series, 16 in the Lower Limestone Shale, 41 in
the Carboniferous Limestone, 7 in the Yoredale, 5 in the Millstone
Grit, 3 in the Lower Coal-measures, 1 in the Middle Coal-measures
(P. scabriculus), and none in the Upper Coal-measures; the genus
(but no known Carboniferous species) passes to the Permian rocks,
and is represented by P. horridus, its last appearance.
The genus Spirifera attains its highest development in this
horizon aleor ; 30 species range side by cide by with the Producta; and
it is well to state also their numerical value in the several horizons :
Calciferous Sandstone 3 species, Lower Limestone Shale 17, Carbo-
niferous Limestone 30, Yoredale rocks 6, Millstone Grit 4, Lower
Coal-measures 4. 2 of the 30 species of Spirfera are Devonian,
Sp. lineata and Sp. Urii; thus 28 species are new to Britain; and
no less than 185 species (British, European, and American) have been
described. The Lhynchonelle of our Carboniferous rocks number
21 out of the 30 European species; and 18 of them are new; the
3 derived from the Devonian are 2. plewrodon, R. pugnus, and
KR. remformis.
The genus Zerebratula begins here to be numerically abundant,
no species being known in the Silurian strata, and the Devonian
rocks yielding only 4 species, whilst 7 species are Carboniferous.
The great development of this genus in the Jurassic rocks surpasses
that of all other Clistenterata; in our own area they apparently
nearly died out or migrated after the Carboniferous epoch, none
occurring in the Trias. The genus Athyris ranges from the Cal-
ciferous Sandstones to the Lower Coal-measures ; A. ambigua and
A, planosulcata are the only species that transgress the Carboni-
ferous Limestone. The genus Atrypa was formerly recognized as
a Carboniferous genus with $ 26 species, which are now relegated to
Rhynchonella, Retzia, and Athyris. Camarophoria, with its 5 species,
belongs to the Carboniferous Limestone ; only C. crumena passes to
the Permian, omitting the 5 intermediate stages or horizons.
Chonetes, only in one instance (under the species hardrensis), ranges
above the Carboniferous Limestone into the Lower Coal-measures,
the whole 15 species being otherwise confined to the limestone
and the shale below.
The significance or importance of Productus as a Carboniferous
genus cannot be overlooked when determining through its species
definite horizons in these rocks. It is ubiquitous; in no region on
the globe, where the Carboniferous rocks are developed, do we not
find “this characteristic shell and in vast abundance—in the Polar
regions, Australia, New Zealand, Van Diemen’s Land, India, Ame-
rica (in 15 States), throughout Europe, and in Africa.
The Carboniferous Brachiopoda consist of 20 genera and 175
ANNIVERSARY ADDRESS OF THE PRESIDENT. 215
species; and 7 of the 8 horizons possess them: 9 genera and 18
species occur in the Calciferous Sandstones of Scotland; 11 genera
and 380 species range through the thin-bedded Carboniferous Lime-
stone Shales, or the Lower Limestones ; 14 genera and 172 species
have been collected and named from the Carboniferous Limestone
alone; 10 genera and 31 species are from the Yoredale rocks and
Upper Limestone Shales; 11 genera and 24 species are Millstone
Grit; the Lower Coal-measures yield 9 genera and 18 species, and
the Middle 3 genera and 3 species. We know of no Brachiopoda in
the Upper Coal-measures. The whole group, with every species, has
been exhaustively worked out by T. Davidson, Esq., F.R.S., in the
volumes of the Palewontographical Society; nothing is left undone
by that distinguished brachiopodist, whose labours in this field of
paleontology are universal. To Mr. Davidson we are indebted for
the highest research into the morphology, history, and classification
of this most difficult class of Mollusca.
S ce} 3 a
Se te ahve | Ae ene
“eb S Si op g 3
= S @ oO q 3
eo oD) i FL <q oe)
Wamarophoria ..... .....-.-.0.00+. 4 I 3 1 3 12
(CIMOIEUES) GARR agROsO SHORE EE Cn Ea rOnnE 12 10 13 5 28 68
aa asl ccfeine suc es atevernasecs 2 2 3 2 3 12
(CONTTHENT noo SU OSB ESB LORE Eee eee 2 Eve if we 3
IDET) scShSe algae Ree ee eee ae 2 1 2 11 14 30
HUMAN s cacecs vcveeecanese 5 4 3 3 8 23
USHER eae as cel sbeaeeke adlead 7 4 8 8 25 52
FEPROCHUICEUSW grced tes eececs otaneine 45 32 28 47 | 109 | 261
ulaymich Onell se sscce see sencsecees 17 3 11 11 36 78
IRCIVAG) ” Goh hee pe Cen EeEe eae Se acer 3) I 1 3 12 20
SUMMON Ree ccaccecvcses-<c seen 40 21 30 48 | 108 | 247
OPUMECEINA fcc edcc es ccleuer eset ee 3 5 5 3 9 29
Streptorhynchus .................. 4 7 5 3 10 29
BRET EMAL UN AN aici. a's cesses credo +a 4. 3 2 8 26 43
150 94 | 115 | 153 | 891 | 908
The preponderance of the two genera Productus and Spirifera is
a great feature in the Carboniferous rocks. Chonetes, Ahynchonella,
and Orthis follow in importance so far as the number of species lends
significance. Chonetes and Productus make their first appearance in
these rocks, and, with Leizia, Streptorhynchus, and Cyrtina, dis-
appear at the close of the period. 5 genera and 6 species of Bra-
chiopoda pass to the Permian; they are Camarophoria globulina,
Phill., C. Schlotheimt, V. Buch, Discina Konincku, Geinitz, Lingula
Oredneri, Geinitz, Spirifera Clannyana, King, and Spuriferima cris-
tata; and beyond 2 species of Ostracoda I know no other connecting
or transgressive species than the above; in other words, only 8
species of all orders pass to higher rocks out of the Carboniferous
q 2
216 . PROCEEDINGS OF THE GEOLOGICAL SOCTETY.
system. Even the Rhizopoda (Foraminifera), which have so wide a
distribution in time, occur not beyond the limits of this formation.
Lamerirsrancuiata.—Monomyaria*. This group and the Dimy-
aria united number no less than 54 genera and 415 species. The
Monomyaria, up to the present time, are represented by 10 genera
and 179 species, 103 of which belong to the genus Aviculopecten, 28
to Avicula, Pinna 6, Posidonomya 12, Pterincea 4, Pteronites 9, Stre-
blopierra 3, Gervillia 2, Inoceramus 4, Loma 2, and Pinna 6. The
Calciferous Sandstones of Scotland and Northumberland have yielded
3 genera (Avicula, Aviculopecien, and Pteronites) and 13 species;
the Lower Limestone Shales, or Lower Limestones, 5 genera and 64
species; the Carboniferous Limestone 11 genera and 151 species;
the Yoredale rocks 4 genera (Avicula, Aviculopecten, Pinna, and
Posidonomya) and 14 species; the Millstone Grit 3 genera (Avcula,
Aviculopecten, and Posidonomya) and 11 species; the Lower Coal-
measures 3 genera (the same) and 13 species; 4 species of Aviculo-
pecten occur in the Middle Coal-measures ; and 1 (Aviculopecten papy-
raceus) is the only form in the Upper Coal-measures. The species
having the longest range are Aviculopecten alternatus, A. gentilis, A.
granosus, A. papyraceus, A. quadratus, A. scalaris, and A. variabilis,
Posidonomya Becheri, P. lateralis, and P. membranacea. The species
of the genera Pteronites, Pterinceea, Streblopterra, Posidonomya, Pinna,
Avicula, and most of the Aviculopectines are chiefly from the Car-
boniferous Limestone. We may assume that the largely represented
eroup of the Aviculopectinidz possessed much the same bathymetrical .
range as that of the genus Pecten in our modern seas; the same with
Pinna and Posidonomya. Indeed it would appear, from the per-
sistency of the vertical range of the group Monomyaria, that no
general depth governed their habit ; for only 14 species out of the 178
range above the Carboniferous Limestone and Yoredale beds. 10 are
named above ; and the following 4 may complete the species—Avicu-
lopecten fibrillosus,A. obtusus, Posidonomya Gibsoni,and Pinna spatula.
The Table also expresses the number of species that are in the Mill-
stone Grit and Coal-measures included here. The magnitude of the
Monomyarian group is sufficient reason for treating it separately,
especially considering that one genus alone (Aviculopecten) is repre-
sented by 103 species.
* T retain this term here, including in it only the Asiphonida, represented by
the Ostreidee, Aviculide, and Pectinide.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 217
|
~ | :
Gen MEE < A S
S S a 1] ay
Beco ties mi <4
A STCITT S E Se Oa 2 ed |
Piriatilen ete Re ie 25h dg 16 10. i 2S ulna ni moe:
EVICBIGNECEEM | conc cne-neneeecse> 2 48 50 80 | 33 40
PD YETSTTLTIES Re ae + its 2 lsc 5
IRRECCEATINUS, cc cteccs cs icc sciessecest ae 4 1 1
LUTTE O) Seinen i OC 2 | nef} Al
LEGO. GOk ae eRe Eee eee , 1 ee ees
"PATER Rtn aae ene ae 5 5 3 | 6
EGRIGOHOMYS ....,..0.sncereceese 8 2 8 5 J.
ETRE et ecm cccoes snes cuecete i x2) aeelitysee 9
PETEPOMICES Sones ec sscsccbcveccotess 3 6 7 be 2
85 74 | 186 67
pa
eS
Oo
The preponderance of species in one genus, as in Aviculopecten,
is unexampled in any other British formation. 150 species occur in
Britain and Europe; 50 have been described from America, and all
differ from our forms. The species occurring in the Belgian Car-
boniferous rocks are known to us through the researches of De
Koninck. In Ireland, mainly through the researches of M‘Coy
and Baily, the Integropallialia appear to have been exhaustively
recorded. The genus Avicula, in the Irish Carboniferous rocks,
numbers about 23 species, Aviculopecten 80, Pecten 5, Pteronites 5,
Posidonomya 8, Pierinea 3, Pinna 5. Scotland: Avicula 10, Avicu-
lopecten 50, Pinna 4, Posidonomya 2, Pteronites 6. England: Av-
cula 16, Aviculopecten 48, Pinna 5, Posidonomya 8, Pieronites 3, and
Pterinea 1. These comparisons are important, as showing geogra-
phical distribution as well as age. The collective fauna illustrating
this group in all Kurope beyond Belgium does not exceed 50 species,
showing either want of research or the small development of the
Carboniferous rocks east of Rhenish Prussia.
LAMELLIBRANCHIATA.— Dimyaria*.—No less than 43 genera and
245 described species occur in the Carboniferous rocks, the largest
number being in the Carboniferous Limestone (80 genera and 182
species); the underlying Lower Limestone and Shales yield 23 genera
and 103 species; and the Calciferous beds of the north of Kngland
and Scotland 17 genera and 38 species; only 9 species are Yoredale.
Many species are necessarily common to the three lower horizons ;
but the faunal contents are as stated. The Coal-measure species will
be noticed in their place.
Thus the united British Lamellibranchiate (or Pelecypod) fauna
numerically reaches 54 genera and 424 species, 179 being Mono-
myarian Asiphonida (Integropallialia) and 245 Siphonida (Sinu-
pallialia). Hitherto I have not mentioned the Coal-measure Dimy-
* 18 families, including the Arcidz, Trigonid, and Unionida.
218 PROCEEDINGS OF THE GEOLOGICAL SOOIETY.
aria, or those occurring in the Millstone Grit and Lower, Middle,
and Upper Coal-measures. With the exception of the Lower Coal-
measures, which have yielded 12 genera and 42 species, the three
remaining horizons are comparatively poor, as would be anticipated
from the estuarine condition or nature of the deposits. Anthracosia,
Anthracoptera, Aximus, Ctenodonta, Edmondia, Modiola, Myacites,
Myalina, and Schizodus are the genera that characterize the Coal-
measures, or beds above the Yoredale series.
6 genera and 9 species are all that are known from the Millstone
Grit; the genera are Anthracosia 2 species, Aanus 1, Ctenodonta 3,
Edmondia 1, Lunulacardium 1, Myacites 1.
The genera in the Lower Coal-measures, 14 with 44 species, are
still more estuarine in habit, many allied to the Unionide and
Myadz—Anthracomya 5 species, Anthracosia 6, Anthracoptera 2,
Axinus 2, Conocardium 1, Ctenodonta 6, Edmondia 3, Leptodomus 1,
Modiola 4, Myacites 4, Myalina 6, Pleurophorus 1, Pullastra 1,
Schizodus 2. The Middle Coal-measures have, as yet, only yielded
4 genera and 16 species—Anthracomya 6 species, Anthracosia 6,
Anthracoptera 2, and Myalhna 2 species. The Upper Coal-measures
contain the same 4 genera with 11 species. The above, with the
table of distribution, clearly shows the changes from the deeper-sea
fauna of the Limestone series to the shallow and estuarine accumu-
lations of the Coal-measures, the gradual dying-out of those genera,
essentially dwellers in clear and deep water and with associated
sedimentary matter, as well as the almost total extinction of the
molluscan fauna with the elevation of the sea-bed, a few genera
only living on into the Permian sea.
The accompanying Table gives the numerical value of the species
of 18 of the chief Dimyarian genera out of 43 for England, Scot-
land, and Ireland; also Belgium, for comparison, which is the only
country in Europe where the Carboniferous rocks (Lower series) are
well developed. The researches of Prof. De Koninck, of Liege, have
afforded me data for this column. I have before stated the small
number of known species in the European area beyond Belgium ; to
show, however, the relationship between the American fauna and
our own, I have appended a column also, which shows excess in the
number of species in most of the genera. Such holds good with the
older Paleozoic genera also; but, through the flora and Mollusca of
the Coal-measures, America and Scotland are intimately associated,
and, in a similar but less degree, Ireland,
ANNIVERSARY ADDRESS OF THE PRESIDENT. 219
Table of 18 of the chief Carboniferous Genera, showing their specific
or numerical value through the five areas or countries named.
| | [mel
oe dies : 5 Oo |
ElElglelgig.
Genera. eh ot So lcen ine lee
q s 9 | 'o ee
Bla ae |Alsai6
Allorisma (Myacites) ...... 6} 3] 4 28 | 41
ATC APACOINYA.......00ss-000- Salas 2 | 13 |Chiefly Coal-measures
(6 species).
RIUBEAEORIG) <.650.5 00.0 20200- 10; 9 23 | 8 | 50 | Ditto (6 species).
Lacs, 2 ee AT SOn StOn ke ht 44
LAShit =e Rel ae 100 Sta Et
Cardiomorpha ............... 9} 6| 5]} 86} 18 | 69
Conocardium .........:..... Gullean Ol (Ss) 39
EGtemodouta, <.:.......<...-.-. 11 | 15 | 15 | 9 | 34 | 84 | 6 Coal-measures.
Cypricredia. ....-............. eo OM 1Gy TL os
JSC ES Nit 12 eee 10 | 10 | 12} 2 | 25 | 59 | 8 Coal-measures.
LG) A 10; 8} 12]... | 5 | 35 |4 Coal-measures.
BURY EMBs soa. -cas-..eesees 3; 2] 3] 380] 6} 44
WAM eee. 32-2.--.02.-.00- 6; 9; 1| 3] 18 | 37 |6 Coal-measures.
Sanguinolites................ LOv) 20) | 1645327 |-68
SCLNIZ00 si 3| 8] 7]... | 13 | 31 | 2 Coal-measures.
BCAGWHEMED -20.2.2000s00.000- ees | Bani ak 6 | 15
i Timrce. ——————— Were era omni orl oul t4
SL. TUT 3A Ease eens LST PRG at ha bern
| 106 /102 115 [171 [222 716
Sorznoconce1a.—6 species of Dentaliwm are known ; but none pass
above the Carboniferous Limestone. D. priscwm is the only species
that occurs in 3 horizons—the Calciferous Sandstones, Lower Lime-
stones, and Carboniferous Limestone. JD. scoticum is only found in
the Calciferous Sandstones; the remaining 4 belong to the Carboni-
ferous Limestone, and do not range higher.
GaAsTEROPODA.—223 species and 29 genera, all belonging to the
division Holostomata of the order Prosobranchiata, constitute the
univalve fauna of the Carboniferous rocks. All the genera (29) and
202 species occur in and range through the Carboniferous Limestone ;
or nearly every species occurs in this horizon. 16 of the 29 genera
are distributed through the Carboniferous rocks of Europe and
America, and are therefore of zoological as well as stratigraphical
value. I give the following Table of these genera to accompany
that showing the distribution of the Lamellibranchiata (Dimyaria) ;
by comparison with the molluscan fauna of Europe and America
we may hope to obtain some clue relative to the migration and dis-
persion of the Mollusca from some original area. These 16 chief
genera are represented in England by 176 species, in Scotland by
90, in Ireland by 111, in Belgium (chiefly through De Koninck) by
176, and in the American Carboniferous rocks by nearly 200 species.
This generic relationship with America is important as determining
similarity of bathymetrical conditions, temperature, and food, and con-
nexion through coast-line or land now lost. 9 genera and 21 species
nt
220 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
occur in the Calciferous Sandstone—Huomphalus 4 species, Lacuna
1, Inttorina 2, Loxonema 2, Macrocheilus 4, Murchisonia 3, Natica 1,
Naticopsis 1, Pleurotomaria 3.
The Lower Limestone Shales contain 50 species, which, with one
exception (Turbo appropinquans), are also those of the Carboniferous
Limestone above; or 49 of the 50 occur also in the massive lime-
stones.
The Yoredale beds (the Upper Limestone Shales of some authors) are
poor in Gasteropoda; only 7 genera and 10 species appear to be known.
Clearly this must be the result of imperfect collecting rather than
of almost total absence of species. We know that both the Lower and
Upper Limestone Shales are impure argillaceous limestones, and not
favourable to the presence of the Mollusca at the time of deposition
or to the preservation of organic structure afterwards: but we see here
the 7 genera only represented by 10 species; they are :—Huomphalus
catillus, Sow.; Loxonema constricta, Sow.; Macrocheilus curvilinea,
Phill.; Jf. imbricatus, Sow.; M. rectilinea, Phill.; Murchisonia
fusiformis, Phill.; Naticopsis plicistria, Phill.; Plewrotomaria lim-
bata, Phill.; P. twmida, Phill.; and Yurritella tenwistria, Phill.
The Millstone Grit, as we should expect, contains but a small
Gasteropod fauna; such arenaceous deposits suit not the habits of
this group of Mollusca; only 3 genera and 3 species are known—
Natica variata, Phill.; Pleurotomaria limbata, Phill.; and Murchisonia
fusiformis, Phill. The Pelagic Cephalopoda in the same beds, as we ©
shall see, number no less than 33 species; but the sandy and muddy
beds of the shore was not their habitat; they are not such good wit-
nesses in the beds in which they are found as the ordinary Lamelli-
branchiata and Gasteropoda. The Lower Coal-measures alone yield
Gasteropoda; none are known either in the Middle or Upper. 7 genera
and 19 species are recorded from this division :—Huomphalus Glover,
Brown; Juttorina obscura, Sow.; L. solida, De Kon.; Loxonema
galvam, Baily; L. minutissema, Baily; L. Owen, Brown; L. reticu-
lata, Brown; Macrocheilus, 4 species ; Natica vetusta, Sow.; Nats-
copsis plicistria, Phill.; Plewrotomaria limbata, Phill.; P. usocona,
Sow.; Zurritella, 4 species.
Middle Coal-measures none.
Upper Coal-measures none.
ANNIVERSARY ADDRESS OF THE PRESIDENT. 221
Geographical Distribution of the Gasteropoda through
16 characteristic Genera.
| | |
ne] ne) ra osteo
| Ae es ieeeceices |
SPE. Nishi 1 oes oc Ree ae | =
<3) 2) Ss ea bales 6
“ESET TOL a eae ins ee 6 5 8 13 22, 54
CClifiae, | go ree 3 3 4 15 2, 27
BU OMIDMALUES Jt enscnvesseeeses 20 Wi 20 20 23 | 100
LORS ae a a 2 1 os 2 yes 5
WMERCROCMOIUG! { 1. ..0--cc0--00 lesvses 17 8 12 5 19 61
EOWA A oo ea. = cvnon noses sens 12 Na os 5 2 19
RECIEVE)... soc sorcccceccsseees 15 O 6 19 20 67
MUSE TURN coco es ceacccwswecnose 13 9 9 14 16 61
PE AVICOSIS mod. ais o's ox a'view oneiecnt 2 1 3 a mE 6
[ESE 12) ° 5 Seen eee 7 ae 5 6 ay 18
IPMAMICTORMUS, -coceccsecccecccsecsee 4 ee 3 “ss 2 9
IIABYRCHISWID, 2... 05-2 cecc econo sae 9) 2 4 1 + 16
IEIOMEGLOMIATIG «.-5ccscccneeecnseces 46 24 16 59 65 | 210
MIME TOUS 2s oo coc la occecccccevscaecs 6 1 4 aan 2 13
TNS 19)” GA ae i 6 1 4 fy af, 16
| SOS TEL GSIEE: Gea Seo ere 12 i] 13 12 20 68
176 90 | 111 WG. tb 197-2 F750
Preropopa.—The genus Conularia first appears in the Carboni-
ferous rocks in the Lower Limestone Shale, and ranges through all
but the Upper Coal-measures. This genus dies out in the Coal-
measures. Many of the nodules in the “ Penny-stone” of Coal-
brookdale contain fine examples of C. quadrisulcata, Sow., the only
determined species known. An undetermined species occurs in the
Calciferous Sandstones of Woodhall, Scotland. America yields 17
species of Conularia to our 2; our C. quadrisulcata is not known
out of Britain.
Herrrovopa.—Bellerophon and Porcellia (the former with 27
species and the latter 4) exhaust the species in the Carboni-
ferous rocks. At no period in Paleozoic times did so many species
of Bellerophon exist in one horizon. 24 of the 27 species are
found in the Carboniferous Limestone; and 6 of these 24 species
range higher; they are :—JBellerophon apertus, Sow.; B. decussatus,
Flem.; B. Dumonti, D’Orb.; B. hiulcus, Mart.; B. Oldham, Portl. ;
and B. Uru, Flem. 4 species (B. costatus, Sow., B. decussatus,
Flem., and var. undatus, Kther., and B. Urii, Flem.) are Calciferous
or Tuedian species. B. decussatus, B. apertus, B. hiulcus, and B. Urii
range up to the Middle Coal-measures. 5 species occur in the
Lower Limestone Shale; but none are peculiar to those beds. 17
Species are essentially Carboniferous Limestone. The Yoredale
beds have yielded 4 species—B. apertus, B. decussatus, B. hiulcus,
and B. Urn, all species having a long range. The Millstone
222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Grit contains the same forms. The Lower Coal-measures yield the
same, with the addition of B. navicula, B. Oldhamu, and B.
Dumontic; none occur in the Upper Coal-measures—this order,
like all others in the Carboniferous series, dying out at its close, not
to appear again.
The genera Bucania of Hall and Huphemus of M‘Coy are synony-
mous with Bellerophon. Ireland has yielded 21 species of Bellero-
phon, Scotland 15, England 17, Belgium 25, and America 39 species ;
only 19 species range through Europe, 8 of them being British; and
14 of these 19 are Russian.
CrpHatopopa.—No fewer than 169 species are distributed through
the British Carboniferous system. 4 genera and 6 species occur in
the Calciferous or Tuedian beds, 5 genera and 22 species in the Lower
Limestone Shale, 8 genera and 140 species in the Carboniferous Lime-
stone ; 5 genera and 33 species are Yoredale ; 3 genera and 30 species
are Millstone Grit; 3 genera and 24 species occur in the Lower Coal-
measures, 3 genera and 6 species in the Middle Coal-measures, and
1 genus and 2 species in the Upper Coal-measures. These 169 species
represent 8 genera—Actinoceras 1 species, Cyrtoceras 3, Discites 17
(subgenus of Nautilus), Goniatites 59, Nautilus 36, Orthoceras 48,
Poterroceras 3, and Tirigonoceras 2 species.
The accompanying Table of the 8 British genera shows the number
of species in each country, including, as in the two prior Tables,
Belgium and America for comparison, in which it will be seen that
the 169 species, through the 500 occurrences, are thus distributed :—
the number of species in the 8 genera in England is 126, in Scot-
land 63, in Ireland 107, and in Belgium 90. Comparison carried
beyond Europe to America, as before, shows generic affinity through
114 species, hardly a single form being British. All Europe, only
yields 95 species through 11 areas; research and the accident of our
possessing these rocks highly developed is the reason why our mol-
luscan fauna is so extensive.
8
é : : q
rd oo ro 3
BP lik Os lly ee ca ees a
a) 3) 5 a0 ee
WA CEIMOCELAS Ye face sean oe ekeseeenee 1 1 1 1 2 6
Oyrtoceras.:, hiss sc. seeasenlesdwcess 2 3 aie 8 5 18
DIS Cites, Sees. f ee Ne asset eek 10 3 LS idee 1 32
Goniatites 2047 tcacnaneccteeties 59 15 32 25 32 | 163
Nautilus: tin tscccscsecec neuen ea ea: 18 14 21 22 54. 129
Orthoceras /eeerk eee cee Reena eee 33 24 36 29 20 142
IPoteriocerasin. econ ee eee 2 3 2 au Fad a
Tri gOnOGeLrasnnc:t pa scmeedennesee 1 a 1 1 on 3
126 63 | 107 90 | 114 | 500
ANNIVERSARY ADDRESS OF THE PRESIDENT. 223
VERTEBRATA.
Piscrs.—120 genera and 290 species of fish and 26 genera and
33 species of Amphibia compose numerically the Vertebrate fauna
of the Carboniferous rocks. The comparatively rich assemblage of
ichthyic remains in the Old Red Sandstone bears no proportion to the
great increase and development of this class in the Carboniferous
system. Only two orders are represented in the Carboniferous
rocks, viz. the Ganoidei and Elasmobranchi (Placoidez, Ag.), the
Ganoidei through the suborder Crossopterygide by 4 of the 6 recog-
nized families, the Saurodipterini, Glyptodipterini, Ctenodipterini ?
(Dipnoi)*, and Celacanthini. The Elasmobranchi mainly corre-
spond to the Chondropterygide or the Cartilaginous Fishes of Cuvier
(the Holocephali and Plagiostomi of Owen and the Selachia of
Miller).
The distribution and appearance in time of the two orders appears
to have been much the same; the Plagiostomi first appeared in the
Ludlow rocks, the Holocephali through the Chimeroids in the
Devonian rocks of N. America (genus fhinodus of Newberry). The
section Cestraphori of the order Plagiostomi 1s abundantly represented
in the Carboniferous rocks from base to summit, spines and teeth of
the several genera occurring everywhere, although very locally, the
Cienacantht, Gyracanth, Homacantht, Oracanthi, Onchi, and Lepta-
canthi being the most important, and occurring as spines (Ichthyo-
dorulites).
The genera or groups illustrated by palatal and other teeth are
Cochliodus, Deltodus, Psammodus, Petalodus, Otodus, Ctenoptychius,
Cladodus, Glossodus, Diplodus, Helodus, &e. Many of these generic
groups will be greatly reduced under stricter and more complete
research. My duty here is not to criticise, but rather to bring
together for a special purpose the labours of others as at present
received.
The lowest recognized rocks of the Carboniferous system, the
“‘Calciferous Sandstone” of the Scotch geologists, or Tuedian of
Northumberland, confined to the north of England and south-east-
ern Scotland, contains 13 genera and 14 species—Cladodus 1 species,
Cienacanthus 1, Ctenodus 1, Ctenoptychius 1, Diplodus 1, Hurynotus 1,
Megalichthys 1, Nematoptychus 1, Pecilodus 1, Pygopterus 1, Rhadi-
nichthys 1, Rhizodus 2,and Wardichthys 1. Thus, with one exception,
each genus is represented only by 1 species. Surely much has to be
done both with the Ganoidei (8) and Placoidei (5) when better
materials come to hand ; for many of the genera must be established
upon slender grounds.
THe Lower Limestonzs anD SHatEs have yielded 29 genera and
50 species ; and if this lower member be associated with the thick or
* T am aware that Dr. Traquair would remove the Glyptodipterini from the
Crossopterygious Ganoids and place them sectionally in the order Dipnoi (vide
Trans. Roy. Soc. Edinb. vol. xxvii. for the sections and families proposed by
Dr. Traquair).
224 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
true Carboniferous Limestone, the two together would represent 80
genera and 170 species, 17 genera and 22 species being peculiar to
the Lower Limestone Shales. No one can doubt that these dark,
impure, argillaceous limestones were the commencement of the purer
calcareous series above; and paleontologically they cannot be sepa-
rated. Closer research will probably show that the 17 genera now
known to occur only in the Lower Limestones exist in the succeed-
ing series,
Carponirerous Limestonz.—This finely developed group of rocks
in the British Islands, which has received so much attention both
under geological and paleontological aspects, is possibly better
understood than any other division of the Carboniferous system.
The limestone beds known as the Mountain Limestone have yielded
no less than 63 genera and 147 species of fishes; but the Yoredale
series which succeed them yield none ; and only 3 genera and 3 species
are known in the Millstone Grit (Megalichthys Hibberti, Rhizodus
Hrbberti, and Acanthodes Bronni). This sudden cessation or non-
occurrence can scarcely be accounted for on lithological grounds, or
original sedimentary accumulation, such as would be applicable to
the habits of certain genera of the Mollusca. Bathymetrical con-
ditions may have influenced this paucity in the whole fauna of the
Yoredale and Millstone Grit, which is so apparent on inspection of
the Table of Distribution. 38 genera of Placoidei are confined to
the Carboniferous Limestone; and 12 genera of the same order are
from both Lower Limestone Shale and Carboniferous Limestone: on
the other hand, it is remarkable that only 6 genera of Ganoidei are
strictly or essentially confined to that horizon ; they are Acrolepis,
Asterolepis, Coccosteus ?, Cycloptychius, Phyllolepis, and Platycanthus.
(I give them as near the truth as possible, as the species of Ganoidei in
the Carboniferous system are in as much confusion as the Placoidei*.)
As before stated, the Yoredale rocks(Upper Limestone Shale of some
areas) have not yielded remains of fishes. We are in doubt as to the
real position of the Upper Limestones of Durham and Northum-
berland, or what, if any, should be assigned to the Yoredale group.
Nevertheless [ am not aware of any Vertebrata occurring in the
Yoredale beds. The Millstone Grit, as before stated, has only (so
far as I know) yielded 3 genera and 3 species, and these in the
form of scales. |
Lowrr CoaL-MEAsuRES.— Whatever conditions caused so complete
a break in the distribution of the fishes in our area zoologically,
stratigraphically, and geographically during the deposition of the
rocks mentioned, the return of the same genera and many of the
same species in the Lower Coal-measures is equally important. We
have evidence of the remains of 52 genera and 112 species, the
whole composed nearly equally of the orders Placoidei and Ga-
noidei. The numbers may be thus expressed :—In the Lower Coal-
* The Ganoid Fishes are under revision by Dr. Traquair, whose accurate
knowledge of the order will be brought to bear upon their structure and classi-
fication.
ANNIVERSARY ADDRESS OF THE PRESIDENT, 225
measures 32 genera and 50 species of Ganoidei occur, in the Middle
Coal-measures 5 genera and 6 species, in the Upper Coal-measures
6 genera and 8 species. The Placoidei are represented in the Lower
by 22 genera and 40 species, in the Middle by 10 genera and 14
species, and in the Upper by 6 genera and 8 species. Regarding
the Coal-measure fishes as a whole, however, they stand in the Table
as Lower Coal-measures 52 genera and 112 species, Middle 14
genera and 20 species, and the Upper 12 genera and 14 species.
The numerical distribution for Britain and Belgium is—
[ST EG oe 136 species.
seaulands | oss Socey 5... P52) es
Mrclanieey ps 2 ee ad 21) miner
ibelstunyeS a eee ou S. ist) Wagers
‘The Carboniferous system is finely developed in Belgium. 37 of
the same genera occur in the American rocks, 10 being Ganoidei
and 27 Placoidei, the two orders there yielding 240 species.
Amputpra.—Of the 4 orders in the class Amphibia, the Labyrin-
thodontia alone occur in the Carboniferous rocks. 26 genera and
33 species are known in Britain. Without exception they all
occur in one or the other of the divisions of the Coal-measures.
Prof. De Koninck, in his great work (‘ Ann. du Mus. Roy. d’Hist. >
Nat. de Belg.’ tome ii., Faune du Calc. Carb. de la Belg. pt. i.), has
described 29 genera and 44 species, all from the Carboniferous
Limestone. The fauna of the Coal-measures in Belgium is small
compared with that of Britain.
Tue Lowsr-CosL-MEASURE genera are Ainphicelosaurus, Amphi-
saurus, Anthracerpeton, Brachyscelis, Batrachiderpeton, Discospon-
dylus, Dolichosoma, Erpetocephalus, Ichthyerpeton, Keraterpeton,
Lepierpeton, Loxomma, Ophiderpeton, Labyrinthodontosaurus, Lepto-
gnathosaurus, Macrosaurus, Megalocephalus, Orthosaurus, Parabatra-
chus, Pholidogaster, Streptodontosaurus, and Urocordylus.
Tar Mippre-Coat-MpasvRE genera are only 3—Anthracosaurus,
Megalerpeton, and . holiderpeton.
Loxomma and Pieroplax occur in both Lower and Upper Coal-
measures.
We are chiefly indebted to Professors Huxley and Miall for
elaborate researches into the structure and affinities of the extinct
order Labyrinthodontia, a group eminently characteristic of Carbo-
niferous time; for, with the exception of RAinosaurus from the Lias
and the Jurassic Brachyops, no remains of this order have hitherto
been discovered in rocks younger than the Trias.
226 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
TaBLE XVI.— Carboniferous.
———
*UBIMLIOg |
07} 03 ssed an ne oe
yey} soroodg |
*soansvoul-[v0D | .@ ©
soddq ae aN =e OO AR v0 NS av on
"SQITISVOTU-[VOD) | ~@ a o®
AA TO art Oo Av SF ae sa MO
eTPPIAL a mc =e
*SOUNSVOT-[VOD) | ga Glo an
JOMOTT 2% rie SE OA COD Ore may coke Se re nin am mg on an ae
e e . e e pr)
“ITH OUOISTTNAL | aa SS og yeaa HUES Re Pe 22 me an nt a, ae 3 | oe
a 3 Q . ° a
“BpIq, 8TBpat0 X ° rn? XT} ae oe : : : os 2 On n> aeoav “eo : : 2
“QUO SOUT Oa 6 0o ot Ho ot @ : ° > ov 8 At of os te ” ae
snoIE;IUOGIeO nn a ome SN ot ae rie ae 2 S 7 Nr nr ne ae ae 8 ret) (GU OS asi ae
‘OW SOTBYN 9U0JS | ae me CF pq MO AA GORD : ° 2 90 HO Ut ae wa @2 ae mo ROCnE a
-OUI'T -ToMOorT NN aN Ca Cs cb : 2 rN nD “NO a Dale) ; mM e¢ | le
“eudIspUv ; ‘ ; : 3 5 ° iS
enous ee Cy ik} © 08 miet Ar e e A . ov a2 ae =e =a @ ey 305 ay : a
m = c : A
e SoS 1m @ me od ben) set @ om 1a
spdg BS ARPPSeagrVPRRERSS oO PD OD 1O
aR) ma re [ey | mam AN N mw a
: PN ~~ = © © co iis
BIOUOD | SYS) SSS G8) Ge) COGN ca eee “A aR &|3
e
eoreceee
eoveees
°
°
° °
° °
ooreroeeseon
.
.
. °
.
.
eee oseos
°
°
Se eeeeoestoseenses
eoeeesegnten
ry
@eceececoereoree
ate inci : ; 3 Bhp o
pacar: ear ee Sua : aS Ct
Sit iA BS, . CMe mee Orin a) a) o. es 8 (8 he
: Mews ve BF ane : : Ba fi: 2
B street em na: > bi oioi hot @ 2.) 2
wa > “— 2: aM io Sia es Oe hea a 1S of. 'y ee :
m2 od Geach 2 of ob od 8 te 8 gS Be BS
a Sai: 2 8 PP oe RP Be ee
= . Sh MOT tire Sole Cee oni re 2 Oats ort wm 8
PM POP Poi b bob Pop) eR 2
Soweto Boab sb but ues See se
: SENN = yeni: MME aS ec) ae
Ji obo db tpi @ b) e080 Se
ps rs 696.89 8,8 S$ °' gg 2 8&8 6 22> ee
\3 8 SS 3S S386 5 8 Ss 8 0 Zor ee
~~ (2) og Se 2 aC 2 8. 2) © igi fe ommomes is
: om SC) ©) o ey
¢ 8 BHSBsS 2822 BS 8° 822 eee
— 4 oH .
Ja & mae e5aRea48 8 nommhonm <
ne ee ete e Me
“UBIUOARCT WOd AN e's m0 et wo ee tu ow HN Me aa
ANNIVERSARY ADDRESS OF THE PRESIDENT. 227
Tre EXTENSION oF THE OLDER OR Patmozorc Rocks BELOW THE
NEWER oR SECONDARY FORMATIONS.
The position and extension of the Paleozoic rocks beneath the
newer formations of the British Islands is a problem of deep interest,
and is now occupying much attention in consequence of the facts
brought to light by the numerous trials lately made either for the
supply of water or in search of minerals. It may be said that ever
since the remarkable trials for water at Harwich and Kentish Town,
and also the still more remarkable generalizations (almost predic-
tions) of R. Godwin-Austen, Esq., in 1856*, and Prof. Prestwich in
18727, with reference to the possible extension of the Coal-measures
beneath the south-eastern part of England, the minds of pure geolo-
gists have been excited by speculative views, and desires to arrive
at some knowledge of the extension or distribution of old land or
Paleozoic surfaces, so as to restore to the eastward in England the
physical geography of those groups of rocks which now constitute so
grand a feature along the western side of England, Wales, and Scot-
land, but which are lost or covered up beneath the unconformable
newer or Secondary rocks. West of long. 1° 30’ the greater part of
the exposed rocks are Palxozoic, ranging from the Cambrian to the
Coal-measures, their general strike being about N.E. and 8.W.
East of this meridian are Secondary and Tertiary rocks of great
thickness, which doubtless cover the easterly extension of the Pale-
ozoic series towards the European continent. The geographical
changes of land and sea must have been numerous from the time
of the consolidation of the Cambrian sea-bed to the close of the
Carboniferous epoch, the rocks of the latter period being deposited
in depressions and valleys of the older, with succession or position
due to the removal of the subjacent rocks. With the old and wide
extension of these earliest-formed masses we are becoming daily more
familiar. Looking at the physical structure of the south-western
and north-western parts of the British Islands, and the great mass of
the older Paleozoic rocks of North and South Wales, it is evident
that from the Cheviots to Cornwall the oldest rocks in Kurope are
exposed, their eastern extension being hidden. The Northumber-
land and Yorkshire coal-fields down to the latitude of Notting-
ham are covered and deeply buried by the Triassic, Jurassic, and
Cretaceous rocks. South of Nottingham these old land areas are
again exposed; the Charnwood rocks of unknown age, the associated
coal-field of Ashby-de-la-Zouch, with the Warwickshire and South-
Staffordshire coal-fields stand out like islands in the midst of the great
Triassic plain of mid-England; they are the last isolated exposures
or remnants of Paleozoic land seen south of the great Penine axis.
A line drawn from the Malvern range, due south to the Mendips,
and thence to Torquay, will define absolutely the exposed line of
demarcation between the Paleozoic and Mesozoic rocks. The mass
of North and South Wales stands out in bold relief westward
* Quart. Journ. Geol. Soc. vol. xii. pp. 838-4
+t Popular Science Review, vol. xi. p. 241 (1872).
228 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
of the Severn valley. The Old Red mountains and older Silurian
rocks which border the northern edge of the South- Welsh coal-field,
as well as the Devonian promontory of Cornwall and the mass of
North Devon, isolated as they appear to be from the unconformity of
the Secondary rocks, are only apparently so through the great over-
lap. Could we uncover and expose the old Paleozoic floors or land-
surfaces with all their irregularities, doubtless we should find
that the eastern face of the Paleozoic plain would stretch away
under the north-eastern and south-eastern counties and the
German Ocean, the newer rocks filling up the irregularities in the
old land-surface—this denuded plain being either produced by the
eroding agency of the Secondary seas during the slow depression
of the area they then occupied, or previously sculptured and fashioned
into hills and valleys prior to the deposition of the Secondary or
Mesozoic rocks. ‘The Irish Sea, the English Channel, and the
German Ocean are only hollows in the land occupied by the several
seas around the British coasts, any important change in which
would alter our relative position to the continent either to the north,
the east, or the south, and in case of upward movements, would
reveal those accumulations which have gone on since the close of the
Glacial epoch. Could the valleys of the North Sea or St. George’s
Channel, the English Channel, and the German Ocean become again
dry land, we should again be restored to and form part of the great
European plain or plateau, and those stratigraphical masses that are
now abruptly cut off at the coast all round the British Islands would
be traced in broken continuity over their once continuous or origi-
nally connected area. Further, could we strip off all the Secondary
and Tertiary rocks, and reveal or expose the extension of the older
or Paleozoic series towards Germany on the east, and France on
the south, then the vexed question of the old physical geology and
geography (paleography) of Britain and the relation and correlation
of our area with that of Europe would be revealed; the once
continuous terrestrial surface joining us to Europe, and probably
America, on which grew and flourished the flora which furnished
the materials of our coal, could be determined; the probable
relation of the underlying or partly contemporaneous Devonian to
both the Silurian and Carboniferous; the reason for the isolation of
the Old Red Sandstone in different geographical areas, marine in
one area, freshwater in another—the one with a well-defined base
and top, the other having as yet no discovered base, but having a
well-defined passage into the Carboniferous; such and a hundred
other problems would be solved could this old floor be ours to
examine. A rise of a thousand feet would reveal much of all the hidden
older land east of long. 2° W., or all eastward of that which extends
from the southern termination of the Penine chain and Charnwood
Forest ; for we now know that as far south as Northampton, and at
less than 1000 feet*in depth, the Carboniferous Limestone occurs.
Still further south, and but little deeper (1184 feet), the Coal-
measures have been proved at Burford, in each case yielding the
characteristic fossils, the limestone at Northampton being crowded
ANNIVERSARY ADDRESS OF THE PRESIDENT. 229
with 2 species of corals, Lithostrotion irregulare and Lonsdaleia flo-
riformis ; the Coal-measures at Burford with Oyclopteris orbicularis,
Neuropteris, and Pecopteris. By degrees we are arriving at sufficient
data to enable us to judge somewhat of the physiography of these
older accumulations or formations and arriving at their distribution.
The sources of the oldest sedimentary strata will probably ever
remain a mystery; the materials that supplied these oldest British
strata have wholly disappeared ; the extent, distribution, and dimen-
sions of the Paleozoic series all afford indications and proofs of the
vast regions in the north and west which have been thus denuded or
washed away.
This brings me to the consideration of the proof of the extension
of the Upper Silurian and Devonian rocks eastward of the Malvern
chain, the Staffordshire beds (Dudley), and the Bristol Coal-basin,
obtained at no less than five places, if not six; the seventh was
unfortunately never completed.
The oldest rocks yet touched are the Wenlock; they were deter-
mined at Ware, in Hertfordshire, at 795 feet, immediately beneath
the Gault, during the process of boring for an extra supply of water
for the New River Company. These beds dip at an angle of 40° to
the S.E.; consequently their strike is from the N.E. to the S.W.; and
probably the Devonians rest upon them in succession, as they are
known to occur at Turnford, 7 or 8 miles to the south of Ware, and
continuously on to London. No rocks, however, except 1 foot of
Lower Greensand (‘“ Carr stone”), came in between the Silurian and
the Gault—the Devonian, Carboniferous, and all the Lower Secondary
rocks being unrepresented. This feature in the paleogeography
of the eastern region of England, long ago anticipated in some form
by Austen, Prestwich, and Hull, has now been verified, and the age
of the rocks determined. The line occupied by the Wenlock rocks
may be higher or nearer to the north than was hypothetically believed
by the authors above mentioned, but not more so than the
course or strike of the Silurians and Devonians would probably
take, having regard to the position of the Malvern, Woolhope, May-
Hill, and Tortworth Silurians to the west, although the Ware beds
can hardly be referred to the type of Silurian rocks that exists at
the places above named. It will therefore be asked whether this
Wenlock at Ware is of British or continental type; in other words,
ean it be correlated with our Welsh or English Upper Silurian, or is
it of the Ardennes type? Do they constitute a portion of the Staf-
fordshire (Dudley) or Shropshire (Wenlock) Silurians, spreading away
eastwards towards Belgium? or are they a prolongation of the Silu-
rians of Belgium to the west, or a western extension from the con-
tinent? In other words, does this Wenlock at Ware belong to the
edge of another basin or coast-line, an extension from Western
Europe or Scandinavia, or an easterly expansion of the Upper
Silurian of the Silurian area? The facies of the fossils and the
characters of the rock in all essentials are decidedly British; yet
there is much resemblance to the Scandinavian fauna, a prolongation
of the rocks containing which is by no means impossible or impro-
VOL. XXXVII. if
230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
bable. Onthe whole, however, I am inclined to regard the Wenlocks
under Ware as part of the continuous and old denuded Upper Silurian
surface of those rocks now conspicuously exposed in Herefordshire,
Shropshire, and Worcestershire. In direct E. and W. line, and latitu-
dinally, the Wenlock rocks of Malvern, Woolhope, and May Hill may
(under the view of continuity) claim connexion; but I regard the
Ware fossils as having more affinity with the Wenlock-Edge group,
or that series which underlies the western side of the great mass of
the Old Red Sandstone.
The fossils also equally resemble those of the Wren’s Nest at
Dudley, where the dull earthy limestones as well as the crys-
talline ones (as at Ware) occur. The 33 species of fossils noticed
in the cores at Ware are species for species identical with those of
the Wenlock Edge or the Wren’s Nest (Dudley). Could we remove
the overlying Mesozoic series between Ware and Burford, and again
expose the Coal-measures known to occur there at the depth of
1180 feet, then should we better understand the thinning-out of
the Triassic and Jurassic series eastwards towards this Silurian
ridge or plateau. We can hardly .now doubt the extension of
the Burford Coal-measures, in all ‘probability terminating against
the Silurian or Devonian series in the: Ware region, at Turnford,
and near London.
To what distance rocks of these or older date may occur north of
Ware further research alone can:decide. We have, therefore, under
the so-called London basin an axis of Palzeozoic rocks, two divisions
of which are known, the Upper Silurian and Devonian. The Lud-
low rocks may be expected to occur under or a little south of
Hertford ; for, as we shall see, the Devonians set in between Ware
and Turnford, and probably occupy the entire area between that
place and London, where it is now well known they occur under
Tottenham Court Road. The boring at Ware was carried down
797 feet and into the Wenlock beds to the distance of nearly
50 feet, or, to give particulars :—Gravel 14 feet, ‘Chalk 416 feet,
halk-marl 128 feet, Upper Greensand 77 feet, Gault 160 feet, and
Lower Greensand (Carr stone) 1 foot; the boring was continued
for 50 feet in the Wenlock Limestone, and without the intervention
or occurrence of the Devonian. We are thus justified in stating
that the old Paleozoic land-surface composed of Devonian and
Silurian rocks occupies much of Middlesex and Hertfordshire at the
mean depth of 970 feet; they probably extend westward to the
exposed Silurian, Devonian, and Carboniferous areas of Cornwall,
Devon, and Wales. Harwich, which lies 80 miles to the eastward
and 10 miles further north, and probably on the same strike, has
revealed Paleozoic rocks at a depth of over 1000 feet ; but the age of
these Harwich dark clays or shales was never clearly made out.
This question of the depth and geographical extension of these oldest
rocks is seldom practically tested ; for no mineral wealth of sufficient
value occurs below the Coal-measures (Upper Palseozoic) to induce
trial or experiment; and but for the purpose of obtaining water
pure and in quantity, it is questionable if this problem would have
ANNIVERSARY ADDRESS OF THE PRESIDENT, 231
been solved (at present at least); had the Lower Greensand oc-
curred in its normal condition as a water-bearing stratum, or even
had the Upper Greensand (above the Gault) yielded water in quan-
tity, neither at Messrs. Meux’s, at Turnford, nor at Ware should we
have touched the undoubted and unequivocal Devonian and Silurian
strata. Few give thought to or are aware of the difference that
exists in the thickness of rocks of the same age in different yet not
very remote localities. In Britain the Cambrian and Lower Silurian
deposits are from 20,000 to 30,000 feet in thickness, whilst in
Sweden and Russia their representatives or equivalents in time
rarely if ever exceed 1000 feet.
This difference is and was probably due to the form and nature of
the Pre-Cambrian land on which the newer Cambrians and Silurians
were deposited; for there cannot be any doubt that such Pre-
Cambrian rocks did and do exist, and were and are widely extended,
although concealed over the present known European area, and that
their existence was connected with a probable great geographical ex-
tension westwards of the British Islands. The plateau governed by
the 100-fathom level that surrounds the British Islands is part of
this extension, on which all our physical changes have taken place.
Probably the crystalline rocks of Scandinavia, parts of North Wales,
North-west Ireland, St. David’s, and the Hebrides are exposed areas
of this Pre-Cambrian stage of the highest antiquity, and were covered
on their submerged and denuded masses by the Longmynd, Harlech,
ad St.-David’s rocks, which in their turn were succeeded in
some areas by the Lingula-flags, the Tremadoc, and Arenig, life-
groups of antiquity so high that we have no formula to express their
age, or when life first appeared in the seas of the British Islands.
As yet we have no evidence relative to these formations occur-
ring eastward of the Penine chain, of which Charnwood, Ashby-
de-la-Zouch, and the Warwickshire coal-field are the most southerly
exposures ; but we have lately unexpectedly determined the presence
of the Carboniferous Limestone below Northampton at the depth of
890 feet*. This has carried still further south the Penaine axis,
and would lead us to expect that between Northampton and the
exposed Coal-measures of Atherston and Nuneaton an extended coal-
field may occur. What relation the Burford coal on the south may
have is conjectural only; but I am disposed to regard the whole as
one greatly extended coal-tract. We must now regard the Carbo-
niferous Limestone of Northampton in longitude 1° 30’ W. as the
most easterly known in England; and no Triassic rocks cover this
limestone, a few feet only of undeterminable rocks occur between it
and the Lower Liast. Whether the New Red hasthinned away entirely
here, or it happens to be accidentally absent, is a question; but at
Burford on the same strike and relative position there is a consider-
able thickness of Triassic rocks, and to the N. and N.W. also every-
* Jn the cores brought up I determined the presence of Lithostrotion junceum
and Lonsdaleia floriformis in abundance.
+ The cores brought up are 15 inches in diameter. This great undertaking,
as well as those at Turnford and Chatham, were carried on by Messrs. Docwra
and Gulland with their new machinery.
232 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
where. The Upper Devonian beds were first determined by myself
at Messrs. Meux’s ; they are of the true N. Devon and N. Cornwall
Devonian type—dark chocolate-coloured semi-slates containing the
characteristic shells Spirifera disjuncta and Rhynchonella cuboides
&c. This discovery solved the problem of the existence of Paleeozoic
rocks at an accessible depth under London, and of the absence of
the Jurassic series. Immediately above the Devonian occurred the
Lower Greensand, abnormal in all conditions save the never-failing
test of fossil remains, and what few occurred left no doubt as to the
age of this at first somewhat doubtful rock. Trigonia aleformis,
Cardium Hillanum, Trochocyathus Harveyanus, and Cerithia, &e.,
added to the general facies, immediately settled the question of age ;
neither of the other four borings exhibited any signs of the true
Lower Greensand. At Ware and Turnford the Gault rested upon
from 8 to 10 inches of theCarr stone, and this was all that represented
the Neocomian rocks beyond the 65 feet of chalky oolitic subcal-
careous abnormal Lower Greensand; all the borings show that the
Neocomian (Lower Greensand) is interrupted on the north by the
underground Paleozoic ridge. The geographical extent or surface-
area occupied by the Devonian of North Devon between the Pilton
beds on the south and the Linton beds on the north (15 miles),
where we believe we have the full thickness of the whole series, is
as near as possible that known to occur between London and Turn-
ford, assuming that the strike of the North-Devon beds is directly
towards the London area, and thence on towards Belgium and the
Rhine (Eifel and Coblentz). The Devonian cores brought up at
both localities (Tottenham Court Road and Turnford) yielded the
same characteristic fossils; and the beds dipped at the same angle
at both places, 30° $.H.—the plane of the old land-surface being
1148 feet below London, and 980 feet below Turnford, showing a dif-
ference in level of 168 feet, due either to dip or denudation. I should
believe the difference was due rather to denudation along or over a
given plane striking from 8.W. to N.K. Where the junction of the
Upper Devonian and Wenlock rocks may take place between Turn-
ford and Ware it is difficult to say ; but if we infer that the Ludlow
and Lower Devonian beds occur above the Wenlock, dipping south
between Ware and Turnford, then there is little room for them, and
the Upper Devonian must cease at no great distance north of Turnford.
Looking at the thickness of the Lower Devonian in North Devon, and
regarding it as maintaining the same in its strike under Wiltshire,
Buckinghamshire, Middlesex, and Hertfordshire, there is room in
the 8 miles from 8S. to N. at the dip of 30°S. for the presence of the
Lower Devonian and Ludlow. We need not assume that the Lud-
low beds do cecur, any more than we should expect to find the great
sandy and gritty group of the Foreland, whatever it may repre-
sent. The old land-surface, therefore, of Devonian and Old Red
Sandstone of the southern half of England must have extended from
near Yarmouth (lat. N. 52° 50’), descending by a gentle southerly
curve to about Leighton Buzzard, thence 1ising to the Wenlock pro-
montory, and again sharply deflected S.W. to Milford Haven, and
ANNIVERSARY ADDRESS OF THE PRESIDENT. 233
on under the Bristol Channel to Cornwall, all east of the Mendip
Hills being now covered by the Secondary and Tertiary strata—
thus, I think, showing that a widely spread floor of these Paleozoic
rocks occurs under the extensive region of the southern half of
England, and which could as easily be shown to occur in the north
and in Ireland, but under different conditions.
Now that the Ware Upper Silurians have been proved to dip to
the south, we may anticipate the occurrence of the more ancient or
lower series further north towards Cambridge, Huntingdon, and
Peterborough. Whether in their extension northwards they may
be of Scandinavian type we can only surmise, unless the Westmore-
land and Cumberland Silurians pass under the unconformable and
overlapping Carboniferous group of the Penine chain as a con-
tinuous floor or old surface to the south.
Since the determination of the existence of the Devonian rocks
north of the Thames to Turnford, and of the Upper Silurian at Ware,
below the Cretaceous rocks at the depth of 800 feet, our views rela-
tive to the distribution of the Coal-measures have materially altered.
It is clear that all the stratified rocks between the Silurian and Gault
and the Devonian and Gault are wanting or not represented ; in other
words, the whole of the Carboniferous, Triassic, and Jurassic rocks,
and the Purbecks, &c. are missing north of the Thames to lat. 52° 10’.
This shows the great unconformable overlap upon the Silurian and
Devonian floor to the west. Had the sub-Wealden boring been
completed, the problem as to extension would have been solved.
Unfortunately for science this undertaking was never completed,
and the problem remained unsolved; the ancient land was not
discovered. We must rest content with the hypothesis of Mr.
Godwin-Austen as to the area where we should expect to find the
Coal-measures, probably ranging, as he suggests, under or north of
the North Downs. Life must indeed have been most abundant and
prolific in the Wenlock sea of the Ware locality; for so rieh in
fossils are these Ware beds that no less than 33 species were
obtained, all belonging to the Wenlock series, furnishing sufficient
data in themselves to establish and determine the age of the rocks
in which they occur.
The five borings in the London area, or within the London basin,
within a radius of 20 miles, Ware being the furthest removed, taking
them in the order in which they were sunk, may be thus enume-
rated :—No. 1. Kentish Town, 1300 feet deep; the London clay
passed through was 350 feet thick, the Reading beds 50 feet, and
the Thanet sands 15 feet, Upper Chalk 250 feet, Chalk-marl 30 feet,
Upper Greensand 10 feet, Gault 60 feet, and 190 feet of red sandy
rock believed to be Old Red Sandstone or a condition of the Devo-
nian; the depth passed through was 1300 feet.
No. 2. The Crossness new ‘well bore-hole about 1030 feet deep.
No London c¢lay proper occurred in this sinking; the alluvial clay
and gravel immediately below the ordnance level. was 20 feet thick,
and rested upon the Woolwich and Reading and Thanet beds, here
about 100 feet thick, the Chalk 620 feet, the Upper Greensand
234 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
33 feet, the Gault 135 feet, succeeded by loose red, coarse, and fine
sand, having all the appearance of the New Red Sandstone, and
resembling the Kentish-Town Red series.
The boring No. 3, the most important in geological results,
was that at Messrs. Meux’s, Tottenham Court Road. The London
Tertiaries here attained to 156 feet, the Upper Chalk 440 feet,
the Lower Chalk and Chalk-marl 215 feet, the Gault and Upper
Greensand 190 feet, the Neocomian (of peculiar type) 64 feet ;
beneath this occurred the Upper Devonian shales at the depth of
1064 feet, with characteristic fossils, Spirifera disjuncta, Hdmondia,
Rhynchonella cuboides, Orthis sp., &e. This was the first indication
of the presence of rocks older than the Neocomian east of North
Devon and north of the latitude of London, clearly showing the
easterly extension of the Paleozoic rocks from the western side of
England, and extending towards Holland and Belgium. This boring
therefore may be considered classical; it has revealed to us what
was surmised intuitively by Mr. Godwin-Austen and Prof. Prest-
wich. ‘Turnford and Ware have revealed other facts of nearly equal
significance, and at the depth of 940 feet and 800 feet.
The 4th boring is that at Turnford, 12 miles north of London,
where the London Tertiaries are 100 feet thick, the Chalk 620 feet,
the Upper Greensand 15 feet, the Gault 135 feet, the Neocomian,
of the Carr-stone type, about 12 inches. We here again prove the
position of the dark chocolate-coloured Upper Devonian rocks
crowded with characteristic fossils; at the depth of 940 feet I
obtained Spirifera disjuncta, Rhynchonella cuboides, Rhodocrinus,
Strophomena rhomboidalis, Edmondia, Pterineea, <Aviculopecten,
Modiola, Avicula damnoniensis, A. texturata, Fenestella, Tenta-
culites, &c.
The 5th trial or boring for water was at Ware, east of Hertford,
and due north of the Turnford boring. ‘The boring commenced
here in the Upper Chalk, which is 416 feet thick, followed by the
Chalk-marl 125 feet, the Upper Greensand 77 feet, and the Gault
160 feet, the Neocomian a trace only (8 inches), and of the Carr-
stone type, resting upon an eroded surface of Upper Silurian Lime-
stone. The probable relation of these beds to the typical Wenlock
series of Wales and Shropshire I have discussed in the earlier
portion of this section. No less than 20 species of Brachiopoda
alone, with 13 other species, occur and are given in the list; and
all were extracted from a core less than 3 feet in length and 1 foot
in diameter.
The species collected were the following :—
I. Protozoa: Ischadites Kenigu, Murch. II. KcurnopErmata :
Periechocrinus moniliformis and Taxocrinus sp. III. Annevipa: Ten-
taculites ornatus, Sow. IV. Crustacta: Phacops caudatus, Brongn.
MottuscaA Bracutopopa: Orthis canaliculata, Dalm.; O. elegantula,
Dalm.; Meristella tumida, Dalm.; Cyrtia exporrecta, Wahl. ; Spirifera
elevata, Dalm.; S. plicatella, Linn. ; Athyris sp.; Orania implicata,
Sow. : fihynchonella cuneata, Dalm.; Atrypa reticularis ; Pentamerus
faleatus, Dalm.; P. linguifer, Sow.; Strophomena euglypha, Dalm. :
ANNIVERSARY ADDRESS OF THE PRESIDENT. 235
S. reticulata, M‘Coy; S. depressa, Dalm.; S. rhomboidalis, Wahl. ;
S. antiquata, Sow.; Chonetes sp.; Leptena sericea, Sow.; L. trans-
versalis, Dalm. Concnirera: Ctenodonta sp.; Pterinea sp. ;
Mytilus mytilimeris, Conr.; Orihonota rigida, Sow. GASTEROPODA :
EHuomphalus rugosus, Sow. Crpnatopopa: Orthoceras attenuatum,
Sow.; O. angulatwm, Wahl.; and Orthoceras sp.
These five borings within the metropolitan area are of infinite
scientific as well as economic value; and in addition the equally
important trials at Burford due west of Ware, and that of North-
ampton N.W. of London, open up important questions as to the
deeply-seated structure of the triangular area having Ware and
Burford at its base and Northampton at its apex. Have we within
the rolls and folds of the Devonian rocks as they strike across
England between latitude 51° and 52° any still undiscovered coal-
tracts? is the Bristol coal-field repeated to the east and N.E. to
Burford, with the underlying Devonian in place to the south-east ?
It would appear so when we regard the bearing and strike of the
older rocks towards the continent. The geological importance and
interest of these borings is their revelation to us of the old Paleo-
zoic land-surfaces, whether coast-lines or tablelands, theoretically
enabling us to reconstruct the physiography of those land-masses,
concealed, yet connected to now exposed areas, whether British,
European, or even American.
February 23, 1881.
Rosert Etuerines, Esq., F.R.S., President, in the Chair.
William Henry Goss, Esq., Rode Heath, Cheshire, and Stoke-
upon-Trent, Staffordshire, was elected a Fellow of the Society.
The following communications were read :—
1. A letter from Dr. John Kirk, communicated to the Society by
the Right. Hon. Earl Granville, dated :—-
‘*H.M Agency and Consulate General,
Zanzibar, December 20, 1880.
‘¢ My Lorp,
‘‘ It may be of interest to record the occurrence here of an
earthquake-shock felt in the island of Zanzibar at 6.58 a.m., mean
time, on the morning of the 18th inst.
« Although the shock was very distinct, no damage appears to
have been done to any buildings in town.
‘Tt is now twenty-four years since a similar shock has been here
noticed ; but on the mainland, especially in the vicinity of Ujiji,
they are both more common and more severe than at the coast.
‘Shortly after the cable was laid between Mozambique and
236 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Delagoa Bay, the communication was suddenly interrupted after
one of these earthquake-shocks, which seems to have caused the
falling in of rocks by which the cable was crushed.
‘“¢ T have the honour to be &c.,
“ Joun Kirk,
H.M. Agent and Consul-General, Zanzibar.”
“ The Right Honourable
Earl Granville, &c. &e.,
London.”
2. “The Permian, Triassic, and Liassic Rocks of the Carlisle
Basin.” By T. V. Holmes, Ksq., F.G.S.
3. 6 On Astroconia Grant, a new Lyssakine Hexactinellid from
the Silurian Formation of Canada.” By Prof. W. J. Sollas, M.A.,
The following objects were exhibited :—
Specimens illustrating the transformation of Spodumene into
Felspars, from Branchville, Connecticut, exhibited by H. Bauer-
man, Esq., F.G.S.
Canine of Deuterosaurus biarmicus, Eichw., from the Upper Per-
mian of Kargalinsk Steppe, Bere exhibited by W. H. Twelvetrees,
Ksq., F.G.S.
Plates prepared for the illustration of the next part of Dr. A.
Fritsch’s ‘Fauna der Gaskohle und der Kalksteine der Permfor-
mation Bohmens.’
March 9, 1881.
Rosert Erueriper, Esq., F.R.S., President, in the Chair.
Robert Thompson Burnett, Esq., Irlams o’th’Height, near Man-
chester; William Erasmus Darwin, Esq., B.A., Basset, South-
ampton ; Charles James Fox, Ksq., 26 South Molton Street, W. ;
and the Rev. T. Granger Hutt, M.A., Sedbergh, Yorkshire, were
elected Fellows of the Society.
The following communications were read :—
1. “ Description of Parts of the Skeleton of an Anomodont Reptile
(Platypodosaurus robustus, Ow.).—Part I. The gens 7%) By Prom
Owen, C.B., F.R.S., F.G.8., &e.
2. “On the Order Theriodontia, with a Description of a new
Genus and Species (4lurosaurus felinus, Ow.).” By Prof. Owen,
CoBS Ban Se EeGes:
3. * Additional Observations on the Superficial Geology of British
Columbia and adjacent regions.” By G.M. Dawson, Esq., D.Sc.,
F.GS.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 237
The following specimens were exhibited :—
Skull of dlurosaurus felinus, exhibited by Prof. Owen, in illus-
tration of his paper.
Incisor tooth of Deuterosaurus biarmicus, Kichw.; and a Repti-
lian canine from the Upper Permian Cupriferous Sandstones of
Kargalinsk Steppe, near Orenburg, exhibited by W. H. Twelvetrees,
Esq., F.G.S.
March 23, 1881.
R. Erxeries, Esq., F.R.S., President, in the Chair.
Rey. Daniel Dutton, Sydney Street, Wellington, New Zealand ;
and Capt. George Ernest A. Ross, 170 Cromwell Road, 8. W., were
elected Fellows of the Society.
The following communications were read :-—
1. “The Upper Greensands and Chloritic Marl of the Isle of
Wight.” By C. Parkinson, Esq., F.G.8. ~
2. “On the Flow of an Ice-sheet, and its connexion with
Glacial Phenomena.” By Clement Reid, Esq., F.G.S.*
3. “ Soil-cap Motion.” By R. W. Coppinger, Esq. Communicated
by the President.
The following specimens were exhibited :—
A large pebble from the Gault of Folkestone, exhibited by J. 8.
Gardner, Esq., F.G.S.
Some recent Centipedes, killed near Upata, 60 miles 8.E. of Las
Tablas, on the Orinoco River, exhibited by G. Attwood, Esq.,
NG:S.
April 6, 1881.
J. W. Horxs, Esq., F.R.S., Vice-President, in the Chair.
Edward F. Boyd, Esq., Moor House, Leamside, Fence Houses ;
Herbert de Haga Haig, Esq., Lieut. R.E., Staff College, Camberley,
Farnboro’ Station; J. C. Margetson, Esq., 2 Spring Hill, Kings-
down, Bristol; Edward David Price, Esq., Collegiate School,
Hounslow; and James Tonge, Esq., Woodbine House, West-
houghton, Bolton-le-Moors, were elected Fellows of the Society.
* This paper has been withdrawn by the author with the permission of the
Council.
VOL. XXXVII. §
238 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
The following communications were read :—
1. “ The Microscopic Characters of the Vitreous Rocks of Montana,
US.” By F. Rutley, Esq., F.G.S.; with an Appendix by James
Eccles, Esq., F.G.8.
2. “On the Microscopic Structure of Devitrified rocks from Bedd-
gelert, Snowdon, and Skomer island.” By F. Rutley, Esq., F.G.S.
3. “The Date of the last Change of Level in Lancashire.” . By
T. Mellard Reade, Esq., C.E., F.G.S.
The following specimens were exhibited :—
Specimens of arsenical silver-ore from Gunnison, Colorado, ex-
hibited by H. Bauerman, Esq., F.G.S.
Rocks and rock-sections, exhibited by F. Rutley, Esq., in illustra-
tion of his papers.
April 27, 1881.
R. Erxeriner, Esq., F.R.S., President, in the Chair.
Samuel Gerrard Kirchhoffer, Esq., M.A., Yately Grange, Farn-
boro’ Station; Arthur Henry Shakespere Lucas, Esq., The Leys,
Cambridge ; and Frederick Thomas Nelson Spratt, Esq., Lieut. R. E.
Clare Lodge, Tunbridge Wells, were elected Fellows of the Society.
The following communications were read :—
1. “On the precise Mode of Accumulation and Derivation of the
Moel Tryfan Shelly Deposits ; on the Discovery of similar high-level
Deposits along the Eastern Slopes of the Welsh mountains ; and on
the Existence of Drift-zones showing probable Variations in the Rate
of Submergence.” By D. Mackintosh, Esq., F.G.S.
2. “On the Correlation of the Upper Jurassic rocks of England
with those of the Continent.” By the Rev. J. F. Blake, M.A.,
F.G.S. Part I. The Paris basin.
3. “On Fossil Chilostomatous Bryozoa from the Yarra-Yarra,
Victoria, Australia.” By Arthur William Waters, Esq., F.G.S.
The following specimens were exhibited :—
Upper molar of an extinct species of Elephant from the Sivélic
Older Pliocene (?), and Plant-remains in ironstone nodules from Coal-
brook Dale, exhibited by E. Charlesworth, Esq., F.G.S.
Specimens from Moel Tryfan and Frondeg gravel-pit, Denbigh-
shire, exhibited by D. Mackintosh, Ksq., in illustration of his paper.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 239
May 11, 1881.
R. Erusrivger, Esq., F.R.S., President, in the Chair.
Joseph Deeley, Esq., Ruabon, North Wales; George Kilgour, Ksq.,
C.E., F.R.A.S., Dutoit’s Pan, Griqualand West, South Africa; and
Roderick William MacLeod, Esq., Bengal Staff Corps, 55 Parliament
Street, W., were elected Fellows of the Society.
The List of Donations to the Library was read.
The following communications were read :—
1. “ Notes on the Fish-remains of the Bone-bed at Aust, near
Bristol, with the Description of some new Genera and Species.” By
James W: Davis, Esq., F.S8.A., F.G.S.
2. “On some Fish-spines from the Coal-measures.” By J. W.
Davis, Esq., F.S.A., F.G.S.
3. “On some specimens of Diastopora and Stomatopora from the
Wenlock Limestone.” By Francis D. Longe, Esq., F.G.S.
[ Abstract. ]
Mr. Longe showed and described some specimens of Bryozoa from
the Wenlock Limestone of Dudley, which he compared with corre-
sponding forms from the Oolites and later periods, and pointed out
the close similarity of the Silurian with the later forms, in respect
of the shape and dimensions of the cells, as well as in the habit of
ccencecic growth.
Alluding to some other Palzozoic forms, assigned to the Bryozoa
under the generic names of Berenicea and Ceramopora, he pointed
out the difference between the shape of the cells in these forms and
those which he had described, and expressed a doubt whether they
should be classed as Bryozoa at all.
On the other hand, he referred to some specimens described by
Professor Nicholson (Ann. & Mag. Nat. Hist. vol. xv. 1875) under
the names of Alecto auloporoides &c. as having the true Bryozoan
cell, and furnishing additional evidence of the existence in the
Silurian seas of forms of Bryozoa which, though very abundant in
the Oolites and at all subsequent periods, were not generally sup-
posed to have existed in the Paleozoic period.
DiscussIon.
The Prestpenr stated that the genus Aulopora had never been
referred to the Bryozoa before, but to the Actinozoa. He demurred
to the use of the term “‘ plant” as applied to the Bryozoa.
The Avruor stated that the object of his paper was to prove that
in the Wenlock beds he had found forms quite undistinguishable
from Stomatopora or Alecto, and Diastopora or Berenicea of later
periods. He had not confounded Aulopora with the Bryozoa.
240 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
4, “On a new Species of Plesiosaurus (P. Conybeart) from the
Lower Lias of Charmouth, with Observations on P. megacephalus,
Stutchbury, and P. brachycephalus, Owen.” By Prof. W. J. Sollas,
M.A., F.R.S.E., F.G.8., &e., Professor of Geology in University
College, Bristol ; accompanied by a Supplement on the Geological
Distribution of the Genus 2 Plesiosaurus, by G. F. Whidborne, Esq.,
M.A., F.G.S.
5. “On certain Quartzite and Sandstone Fossiliferous Pebbles in
the Drift in Warwickshire, and their probable identity with the true
Lower-Silurian Pebbles, with similar fossils, in the Trias at Bud-
leigh Salterton, Devonshire.” By the Rey. P. B. Brodie, M.A.,
E.G.8.
The following specimens were exhibited :—
Fish-spines and Teeth, exhibited by J. W. Davis, ple F.G.S., in
illustration of his papers ; and
Specimens of Diastopora and Stomatopora, onunead by F. D.
Longe, Esq., F.G.S., in illustration of his paper.
May 25, 1881.
R. Ernermer, Ksq., F.R.S., President, in the Chair.
Rey. Tom Bullock Hardern, M.A., LL.M., Burnham Overy, Lynn,
Norfolk, was elected a Fellow of the Society.
The following specimens were presented to the Museum :—The
type specimens illustr ating the ‘* Note on the ‘Tubulations Sableuses’
of the ‘ Etage Bruxellien? in the Environs of Brussels” by H. J.
Carter, Esq., F.R.S. (Ann. & Mag. Nat. Hist. May 1877), who
presented them.
The following communications were read :—
1. “On the Discovery of some Remains of Plants at the base of
the Denbighshire Grits, near Corwen, North Wales.” By Henry
Hicks, M.D., F.G.8. With an Appendix by R. Etheridge, Esq.,
F.R.S., Pres. Geol. Soe.
2. “Notes on a Mammalian Jaw from the Purbeck Beds at
Swanage, Dorset.” By Edgar W. Willett, Esq. Communicated by
the President.
The following specimens were exhibited :—
Specimens of the Reptile Fauna of the Gosau Formation, exhibited
by Prof. H. G. Seeley, F.R.S., F.G.8.; and
Specimens exhibited by Messrs. Hicks and Willett in illustration
of their papers.
a eee
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 241
June 8, 1881.
R. Erurriver, Esq., F.R.S., President, in the Chair.
The Meeting was made a Special General Meeting for the election
of a Member of the Council in the room of the late Sir P. de Malpas
Grey-Egerton, Bart., M.P., F.R.S., F.G.S.
The Presipent announced that the late Sir Philip Egerton had
bequeathed to the Society all the original drawings made from
specimens in the collection of the Earl of Enniskillen for the illus-
tration of Prof. Agassiz’s works on Fossil Fishes. The Society had
long possessed the drawings made for the same purpose from the
Earl of Ellesmere’s collection, and some years ago the Earl of
Enniskillen presented those which had been prepared from speci-
mens in the possession of Sir Philip Egerton. Sir Philip Egerton’s
kind bequest would complete this interesting series.
Mr. Joun Evans remarked that on this, as on so many other
occasions, the Society was deeply indebted to the kindness of the
late Sir Philip Egerton, and proposed that the President and Secre-
taries should be instructed to communicate with Sir Philip’s repre-
sentatives, and to express the gratitude of the Society for this
bequest and their condolence with his relatives on the loss they
have sustained.
Prof. W. Boyp Dawxrys seconded this proposal, which was carried
unanimously.
The ballot fora new member of Council was kept open till 9
o'clock, when Sir John Lubbock, Bart., M.P., F.R.S., was declared
to have been elected.
Grenville A. J. Cole, Esq., Mayland, Sutton, Surrey, and J. L.
Roberti, Hsq., 92 Malpas Road, New Cross, 8.H., were elected
Fellows; and I] Commendatore Quintino Sella, of Rome, a Foreign
Member of the Society.
The following names of Fellows of the Society were read out for
the first time in conformity with the Bye-laws, Sect. VI. B, Art. 6,
in consequence of the non-payment of the arrears of their contribu-
tions :—J. Entwisle, Esq.; R. Koma, Hsq.; W.H. Le Feuvre, Esq.;
C. 8. Mann, Esq. ; Joseph Thompson, Esq.
The following communications were read :—
1. “The Reptile-Fauna of the Gosau Formation, preserved in the
Geological Museum of the University of Vienna.” By Prof. H. G.
Seeley, F.R.S., F.LS., F.G.S8.; with a Note on the Geological
Horizon of the Fossils, by Prof. Edward Suess, F.M.G.S.
2. “On the Basement-beds of the Cambrian in Anglesey.” By
Prof. T. McKenny Hughes, M.A., F.G.8.
VOL. XXXVII. t
242 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
3. “* Description and Correlation of the Bournemouth Beds.—
Part II. Lower or Freshwater Series.” By J. 8S. Gardner, Esq.,
F.G.S.
Specimens were exhibited by Messrs. Seeley, Hughes, and Gardner,
in illustration of their papers.
June 22, 1881.
R. Erurrives, Esq., F.R.S., President, in the Chair.
Thomas Hart, Esq., Richmond Terrace, Blackburn; and David
William Jones, Esq., Coronel, Chili, South America, were elected |
Fellows of the Society. |
Specimens of Tertiary Brachiopods from South Australia, and
three specimens of Mesozoic Belemnites from Central Australia, were
presented to the Museum by Prof. R. Tate, F.G.S.
_ The following names of Fellows of the Society were read out for
the second time in conformity with the Bye-laws, Sect. VI. s, Art. 6,
in consequence of the non-payment of the arrears of their contribu-
tions :—J. Entwisle, Esq.; R. Koma, Esq.; W.H. Le Feuvre, Esq.;
C. 8. Mann, Esq. ; Joseph Thompson, Esq.
The following communications were read :—
1. “ Description of a new Species of Coral from the Middle Lias
of Oxfordshire.” By R. F. Tomes, Hsq., F.G.S.
2. “ Note on the Occurrence of the Remains of a Cetacean in the
Lower Oligocene Strata of the Hampshire Basin.” By Prof. J. W.
Judd, F.R.S.; Sec. G.S. With a Note by Prof. H. G. Seeley, F.R.S.,
3. ‘Description of a Peat-bed interstratified with the Boulder-
drift at Oldham.” By G. H. Hollingworth, Ksq., F.G.S.
4. “Silurian Uniserial Stomatopore and Ascodictya.” By G. R.
Vine, Esq. Communicated by Prof. P. Martin Duncan, F.R.S.,
5. “Note on the Diamond-fields of South Africa.” By. EH. J.
Dunn, Esq. Communicated by Prof. Ramsay, F.R.S., F.G.S.
6. “On a new Comatula from the Kelloway Rock.” By P. H.
Carpenter, Esq., M.A., Assistant Master at Eton College. Commu-
nicated by the President.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. 243
7. “Descriptive Catalogue of Ammonites from the Sherborne
District.” By Sydney 8. Buckman, Esq. Communicated by Prof.
J. Buckman, F.G.S., F.L.S., &c.
The following specimens were exhibited :—
Prehistoric remains (pottery &c.) found by J. B. Andrews, Esq.,
of Mentone, at St. Vallier, near Grasse, in the neighbourhood of
dolmens &c.
Specimens exhibited by Messrs. Tomes and Judd in illustration of
their papers.
t2
ADDITIONS
TO THE
LIBRARY AND MUSEUM OF THE GEOLOGICAL SOCIETY.
Session 1880-81.
I. ADDITIONS TO THE LIBRARY.
1. PreriopiIcaLts AND Pusiicatrions oF LEARNED SOCIETIES.
Presented by the respective Societies and Editors, if not otherwise
stated.
Academy, The. Nos. 425-451. 1880.
The British Association at Swansea, 157, 176, 190.
Nos. 452-478. 1881.
Adelaide. Philosophical Society. Transactions and Proceedings and
Report for 1878-79. 1879.
R. Tate. Anniversary Address, xxxix.—G. Scoular. The Geology of
the Hundred of Munno Para, Part 1, 60—O. Tepper. Introduction to
the Cliffs and Rocks at Androssan, Yorke’s Peninsula, 71.—R. Tate.
The Natural History of the Country around the Head of the Great Aus-
tralian Bight, 94.—R. Tate. Zoologica et Paleontologica Miscellanea,
chiefly relating to South Australia, 129.
——. Royal Society of South Australia. Transactions and
Proceedings and Report. Vol. i., for 1879-80. 1880.
R. Tate. Anniversary Address, 39.—J. E. Tenison-Woods. On some
recent and fossil Australian Selenariads, 1—Otto Tepper. ‘The “ Bay
of Biscay’ Soil of South Australia and its Formation, 91.—J. Hi. Tenison-
Woods. Onsome new Corals from the Australian Tertiaries, 99.—R. Tate.
Description of a new Species of Belemnite from the Mesozoic Strata of
Central Australia, 104.—G. Scoular. The Geology of the Hundred of
Munno Para, Part 2, 106.—R. Tate. On the Australian Tertiary Pal-
hobranchs, 140.—R. Tate. Rock-formations and Minerals in the vicinity
of Peake, C. A., 179.—W. Fowler. Sections of Strata traversed by two
wells at Yarrow, in the Hundred of Clinton, 181.
Albany. New-York State Museum of Natural History. Annual
Reports, Nos. 28 (Museum edition, 1879), 29-31. 1878-79.
Presented by James Hall, Esq., F.M.G.S.
Analyst, The. Vol. v. Nos. 52-57. 1880.
Vol. vi. Nos. 58-63. 1881. -
Annals and Magazine of Natural History. Ser. 5. Vol. vi. Nos.
31-36. 1880. Purchased.
C. Lapworth. On the Geological Distribution of the Rhabdophora, 16.
—A. W, Waters. Note on the Genus Heteropora, 156.—C. Lapworth.
On the Geological Distribution of the Rhabdophora, 185.—H. J. Carter.
=i
ADDITIONS TO THE LIBRARY. 245
On fossil Sponge-spicules from the Carboniferous Strata of Ben Bul-
ben, near Sligo, 209.—G. Cotteau. On the Tertiary Echinida of
Beleium, 246.—R. Etheridge, Jun. Notes on the Gasteropoda contained
in the Gilbertson Collection, British Museum, and figured in Phillips’s
‘Geology of Yorkshire,’ 289.—A. J. Jukes-Brown. The Chalk Bluffs of
Trimmingham, 305.—H. Alleyne Nicholson. On the Minute Structure of
the recent Heteropora neozelanica, Busk, and on the Relations of the
Genus Heteropora to Monticulipora, 329, 414.—A. Agassiz. On Paleon-
tological and Embryological Development, 348.—J. W. Davis. On a
Species of Gyracanthus, a fossil Fish from the Coal-measures, 372.—W.
J. Sollas. On the Flint Nodules of the Trimmingham Chalk, 384, 437.
Annals and Magazine of Natural History. Ser. 5. Vol. vu. Nos.
37-42. 1881. Purchased.
H. A. Nicholson. On some new or imperfectly-lnown Species of
Corals from the Devonian Rocks of France, 14.—R. Etheridge, Jun.
Descriptions of certain peculiar Bodies which may be the Opercula of
small Gasteropoda, discovered by Mr. James Bennie in the Carboniferous
Limestone of Law Quarry near Dalry, Ayrshire, with Notes on some Si-
lurian Opercula, 25.—W. J Sollas. Note on the Occurrence of Sponge-
spicules in Chert from the Carboniferous Limestone of Ireland, 141.—G.
C. Wallich. On the Origin and Formation of the Flints of the Upper or
White Chalk; with Observations upon Prof. Sollas’s Paper in ‘ The Annals
and Magazine of Natural History’ for December 1880, 162.—S. H. Scudder.
Relation of Devonian Insects to Later and Existing Types, 255.—G. C.
Wallich. On Siliceous Sponge-growth in the Cretaceous Ocean, 261.—P.
H. Carpenter and R. Etheridge, Jun. Contributions to the Study of the
British Paleeozoic Crinoids, 281.—H. J. Carter. On the Kunker Formation
of the Alluyium in India compared with the Flint Formation in the Chalk
of England, 308.—H. Filhol. The Bears of the Cavern of Lherm, 428.—
J. W. Davis. On Paleospinax priscus, Egerton, 429.—S. H. Scudder.
The Structure and Affinities of Euphoberea, Meek and Worthen, a Genus
of Carboniferous Myriopoda, 437.—O. C. Marsh. Discovery of a fossil
Bird in the Jurassic of Wyoming, 488.
Atheneum (Journal). Nos. 2748-2774. 1880.
A. C. Ramsay. Address delivered at the Swansea Meeting of the
British Association for the Advancement of Science, August 25, 1880, 263.
—British Association at Swansea, 509.
- Nos. 2775-2799. 1881.
Sir Philip de Malpas Grey Egerton, Bart., M.P., 494.—The Hamad, 817.
Parts 630-636. 1880.
Parts 637-640. 1881.
Barnsley. Midland Institute of Mining, Civil, and Mechanical
Engineers. Transactions. Vol. vii. Part 50. 1880.
T. W. Embieton. On an Outburst of Carbonic Acid Gas in the Roche-
belle Coal Mine, France, 89.
Volo vis Rarts 5Jand 53. “lee:
Basel. Schweizerische palaontologische Gesellschaft. Abhandlungen.
Vol. vu. 1880. Purchased.
Forsyth Major. SBeitrige zur Geschichte der fossilen Pferde——Ph.
de la Harpe. Htude des Nummulites de la Suisse et révision des espéces
éocénes des genres Nummulites et Assilina.—L. Rutimeyer. Beitrage zu
einer natiirlichen Geschichte der Hirsche——F. Koby. Monographie
des polypiers jurassiques de la Suisse.—P. de Loriol. Monographie pa-
246 ADDITIONS TO THE LIBRARY.
léontologique des couches de la zone & Ammonites tenutiobatus (Badener
Schichten) d’Oberbuchsitten et de Wangen (Soleure).—P. de Loriol.
Description de quatre échinodermes nouveaux.
Belfast Natural-History and Philosophical Society. Proceedings for
the Sessions 1878-79, 1879-80. 1880.
‘J.J. Murphy. Lunar Volcanoes, 124.—J. J. Murphy. On the Origin
of Mountains and Volcanoes, 148.—W. H. Patterson. Flint Implements
&e. found at Ballymisert, Co. Down, 165.
Berlin. Deutsche geologische Gesellschaft. Zeitschrift. Band xxxii.
Heft 2-4 (1880). 1881.
W. Pabst. Untersuchung von chinesischen und japanischen zur Por-
zellanfabrication verwandten Gesteinsvorkommnissen, 223.—A. Heim.
Zum ‘ Mechanismus der Gebirgsbildung, 262.—F’. Noetling. Die Ent-
wickelung der Trias in Niederschlesien, 300.—F. Sandberger. Ueber die
Bildung von Erzgangen mittelst Auslaugung des Nebengesteins, 350.—
Hi. Dewitz. Ueber einige ostpreussische Silurcephalopoden, 371.—G.
Stemmmann. Mikroskopische Thierreste aus dem deutschen Kohlenkalke
(Foraminiferen und Spongien), 394.—W. Branco. Beobachtungen an
Aulacoceras v. Hauer, 461.—F. Klockmann. Ueber Basalt-, Diabas- und
Melaphyr-Geschiebe aus dem norddeutschen Diluvium, 408.—P. Grigo-
riew. Der Meteorit von Rakowska im Gouvernement Tula in Russland,
417.—Rothpletz. Radiolarien, Diatomaceen und Spharosomatiten im
silurischen Kieselschiefer von Langenstriegis in Sachsen, 447.—A. Neh-
ring. Uebersicht tiber vierundzwanzig mitteleuropaische Quartar-Faunen,
468.—E. Geinitz. Der Jura von Dobbertin in Mecklenburg und seine
Versteinerungen, 510.—Fr. Pfaff. Hinige Beobachtungen tiber den Loch-
seitenkalk, 536.—Fr. Pfaff. Hinige Bemerkungen zu Herrn Heim’s Auf-
satz ‘ Zum Mechanismus der Gebirgsbildung,” 542.—G. Holm. Bemer-
kungen tiber Illenus crassicauda Wahlenberg, 559.—H. Credner. Ueber
Glacialerscheinungen in Sachsen, nebst vergleichenden Vorbemerkungen
uber den Geschiebemergel, 572.—W. Branco. Ueber die Verwandtschafts-
verhaltnisse der fossilen Cephalopoden, 596.—Huyssen. Uebersicht der
bisherigen Ergebnisse der vom Preussischen Staate ausgefuhrten Tief boh-
rungen im norddeutschen Flachland und des bei diesen Arbeiten verfolgten
Planes, 612.—Jentzsch. Uebersicht der silurischen Geschiebe Ost- und
Westpreussens, 623.—W. Dames. Ueber Cephalopoden aus dem Gault-
quader des Hoppelberges bei Langenstein unweit Halberstadt, 685.—M.
Hoyer. Ueber das Vorkommen von Phosphorit- und Grunsand-Geschieben
in Westpreussen, 698.—H. Kayser. Dechenella, ee devonische Gruppe
der Gattung Phillipsia, 703.—C. Rammelsberg. Ueber die Vanadinerze
aus dem Staat Cordoba in Argentinien, 708.—Max Bauer. Dioptas aus
den Cordilleren von Chili, 714.—Max Bauer. Nochmals die Krystallform
des Cyanit, 717.—C. Struckmann. Ueber die Verbreitung des Renthiers
in der Gegenwart und in alterer Zeit nach Maassgabe seiner fossilen Reste
unter besonderer Beriicksichtigung der deutschen Fundorte, 728.—F.
Wahnschaffe. Ueber Gletschererscheinungen bei''Velpke und Daundorf,
774.—Otto Lang. Ueber den Gebirgsbau des Leinethales bei Gottingen,
799, :
——. Gesellschaft naturforschender Freunde. Sitzungsberichte,
1880. 1880.
K. A. Lossen. Vorlegung und Besprechung von Handstucken und
Diinnschliffen metamorphosirter Eruptiv- bezw. Tuff-Gesteine vom Schma-
lenberg bei Harzburg, 1.—O. Reinhardt. Ueber die zum Subgenus Or-
cula, Held, gehorigen Pupa-Arten und deren geographische Verbreitung,
12.—yv. Martens. Ueber vorspringende Linien an der Innenflache einiger
ADDITIONS TO THE LIBRARY. 247
Muschelschalen, welche die Lage der Kiemen markiren, 22, 59.—
S. Schliiter. Ueber Zoantharia rugosa aus dem rheinischen Mittel- und
Ober-Devon, 49.
Berlin. K6niglich preussische Akademie der Wissenschaften. Mo-
natsbericht. March to December 1880. 1880-81.
Rammelsberg. Ueber die Zusammensetzung des Descloizits und der
naturlichen Vanadinverbindung en itberhaupt, 652. — Rammelsberg.
Ueber die Zusammensetzung des Pollucits von Hlba, 669. — Websky.
Ueber die Krystallform des Descloizit, 672.
d . September and October 1880. 1881.
Websky. Ueber die Krystallform des Vanadinits von Cordoba, 779.
Zeitschrift fiir die gesammten Naturwissenschaften. Band lili.
1880.
K. Pettersen. Scheuerungserscheinungen in der gegenwartigen Lit-
toralzone, 247.—P. Kaiser. F%coxylon bohemicum: ein neues fossiles
Laubholz, 309.—L. Besthorn. Der Kohnstein bei Nordhausen, 340.—
O. Luedecke. Ueber einen Anorthithasalt vom Fujino-yama, in Japan,
410.—O. Luedecke. Ueber Roemerit, Grailich, 417—H. Pohlig. Zur
Beantwortung der Frage nach Entstehung der “krystallinischen Schiefer,”
445.—K. Pettersen. Terrassen und alte Strandlinien, 783.—R. Collett.
Glaciale Mergelknollen mit Fischrest-Hinschlissen aus Beieren im nord-
lichen Norwegen, 839.
Bern. Schweizer Alpenclub. Jahrbuch, XV. Jahrgang (1880), and
Beilagen. Purchased. |
H. vy. Fellenberge. Geologische Wanderungen im Rhonegebiet 1878
und 1879, 268.
Birmingham. Mason Science College. Calendar for the Session
1880-81. 1881.
Birmingham Philosophical Society. Proceedings, 1878-79. Vol. 1.
No. 3. 1879. Presented by W. Whitaker, Esq., F.G.S.
H. W. Crosskey. Notes on some of the Glacial Phenomena of the
Vosges Mountains, with an Account of the Glacier of Kertoff, 58.—T. G.
Bonney. The Structure and Distribution of the Pre-Cambrian Rocks of
Britain, 140.
Bordeaux. Société Linnéenne. Actes. Série4. Tome ii. Livr. 3 et
4, 1879.
Boston. American Academy of Arts and Sciences. Proceedings.
Vol. xv. Parts 1 & 2. 1880.
Boston Society of Natural History. Memoirs. Vol. i. Partl. No.3.
1879.
S. H. Scudder. Palzeozoic Cockroaches: a complete Revision of the
Species of both Worlds, with an Essay toward their Classification, 23.
Occasional Papers. III. 8vo. 1880.
W. O. Crosby. Contributions to the Geology of Eastern Massachu-
setts, 1.
Proceedings. Vol. xx. Parts 2 & 3 (1878-80). 1879-80.
N.S. Shaler. Evidences of a Gradual Passage from Sedimentary to
Volcanic Rocks in the Brighton District, 129. == ©. Crosby. Occur-
rence of fossiliferous Boulders in the Drift of Truro, Cape Cod, 136.—
T. Sterry Hunt. Remarks on the Precambrian Rocks of Great Britain,
248 ADDITIONS TO THE LIBRARY.
140.—W. O. Crosby. A possible Origin of Petrosiliceous Rocks, 160.—
G. F. Wright. The Kames and Moraines of New England, 210.—W.
Upham. Glacial Drift of Boston and Vicinity, 220.—S. Kneeland. On
the Mineralized Phosphatic Guanos of the Equatorial Pacific Islands,
935.—N. 8. Shaler. Notes on the Submarine Coast-shelf, or Hundred
Fathom Detrital Fringe, 278.—M. EH. Wadsworth. Danalite from the
Tron Mine, Bartlett, N. H., 284M. E. Wadsworth. Picrolite from a
Serpentine Quarry in Florida, Mass., 286.—W. H. Melville. Analysis of
the above Picrolite, 287.—J. H. Huntington. On the Iron Ore of Bart-
lett, N. H., 288.—W. O. Crosby. Evidences of Compression in the Rocks
of the Boston Basin, 308.—S. H. Scudder. Probable Age of Haulover
Beach, Nantucket Harbour, 329.
Brighton and Sussex Natural-History Society. Annual Report,
1879-80. 1880. Presented by W. Whitaker, Esq., F.GS.
Bristol Museum and Library. Report of Proceedings at the Tenth
Annual Meeting. 1881.
British Association for the Advancement of Science. Report of the
Fiftieth Meeting, held at Swansea, 1880. 1880.
Everett. Thirteenth Report of the Committee appointed for the pur-
pose of investigating the Rate of Increase of Underground Temperature
downwards in various Localities of Dry Land and under Water, 26.—
W. Pengelly. Sixteenth and concluding Report of the Committee ap-
pointed for the purpose of exploring Kent’s Cavern, Devonshire, 62.—
H. G. Seeley. Report on the Mode of Reproduction of certain Species of
Ichthyosaurus from the Lias of England and Wurtembere, 68.—G. R.
Vine. Report of the Committee appointed for the purpose of reporting
on the Carboniferous Polyzoa, 76.—C. E. De Rance. Sixth Report of the
Committee appointed for investigating the Circulation of the Underground
Waters in the Permian, New Red Sandstone, and Jurassic Formations
of England, and the Quantity and Character of the Water supplied to
Towns and Districts from those Formations, 87.—W. H. Baily. Second
Report of the Committee appointed for the purpose of collecting and
reporting on the Tertiary (Miocene) Flora, &c., of the Basalt of the North
of Ireland, 107.—H. W. Crosskey. Eighth Report of the Committee
appointed for the purpose of recording the Position, Height above the Sea,
lithological Characters, Size, and Origin of the Erratic Blocks of England,
Wales, and Ireland, reporting other matters of interest connected with
the same, and taking measures for their Preservation, 110.—First Report
of the Committee appointed for the purpose of exploring the Caves of the
South of Ireland, 209.—C. H. Perkins. On the Anthracite Coal and
Coal-field of South Wales, 220.—Geddes. Report of the Committee for
conducting Palzontological and Zoological Researches in Mexico, 254.—
J. Gwyn Jeffreys. The French Deep-sea Exploration in the Bay of
Biscay, 378.—W. Whitaker. List of Works on the Geology, Mineralogy,
and Palsontology of Wales (to the end of 1875), 397.—H. C. Bolton.
On the Application of Organic Acids to the Examination of Minerals, 505.
—H.C. Sorby. Presidential Address to Section C, 565.—W. Boyd Daw-
kins. On the Action of Carbonic Acid on Limestone, 573.—F. C. J.
Spurrell. On the Site of a Paleolithic Implement Manufactory at Cray-
ford, Kent, 574.—G. H. Kinahan. On the Hiatus said to have been
found in the rocks of West Cork, 574.—W. H. Dalton. Note on the
Range of the Lower Tertiaries of Hast Suffolk, 575.—J. P. O'Reilly. On
the Relation to be established between Coast-line Directions represented.
by Great Circles on the Globe, and the Localities marked by Earthquakes
= ae
ADDITIONS TO THE LIBRARY. 249
in Europe, 576.—W. J. Sollas. On the Island of Torghatten, 576.—W.
J. Sollas. On a Fragment of Mica Schist, 577.—W. T. Blanford. On the
Geological Age and Relations of the Sewalik and Pikermi Vertebrate and
Invertebrate Faunas, 577.—E. Wethered. On the Sandstone and Grits
of the Lower and Middle Series of the Bristol Coalfield, 579.—J. Prest-
wich. Ona Raised Beach in Rhos Sili Bay, Gower, 581.—J. Prestwich.
On the Geological Evidence of the temporary Submergence of the South-
west of Europe during the early Human Period, 581.—C. Moore. Proofs
of the Organic Nature of Zozoon canadense, 582.—W. J. Sollas. On a
striated Stone from the Trias of Portishead, 586.—W. J. Sollas. On the
Action of a Lichen on Limestone, 586.—W. J. Sollas. On Sponge-
spicules from the Chalk of Trimmingham, Norfolk, 586.—G. M. Dawson.
Sketch of the Geology of British Columbia, 588.—H. H. Godwin-Austen.
On the Post-Tertiary and more recent Deposit of Kashmir and the Upper
Indus Valley, 589.—R. B. Foote. Notes on the Occurrence of Stone Im-
plements in the coast Laterite south of Madras, and in high-level Gravels
and other Formations in the South Mahratta Country, 589.—C. E. De
Rance. On the Pre-Glacial Contours and Post-Glacial Denudation of the
North-west of England, 590—Schaffhausen. On Prehistoric Times in
the Valley of the Rhine, 624.—H. Stopes. On a Paleolithic Stone Imple-
ment from Egypt, 624.—H. Stopes. On a Paleolithic Flint Implement
from Palestine, 624.
Brussels. Académie Royale des Sciences. Annuaire. 1879, 1880,
and 1881. 1879-81.
: . Bulletins. Série 2. Tome xlvi. (1878). 1878.
C. Malaise. Découverte de Brachiopodes du genre Lingula dans le
Cambrien du massif de Stavelot, 58.—C. Malaise et L. de Koninck.
Rapport sur le mémoire de M. A. Renard: “La diabase de Challes,
prés de Stavelot,’ 186, 188.—C. Malaise. Rapport sur le mémoire
de M. L. de Koninck: “Sixiéme notice sur les minéraux belges,” 189,
—A. Renard. La diabase de Challes, prés de Stavelot, 228.—L. L.
de Koninck. Sixiéme et septiéme notices sur les minéraux belges, 240
et 245.—H. Dupont. Rapport sur le mémoire de M. A. Renard: “ Re-
cherches lithologiques sur les phthanites du calcaire carbonifére de la
Belgique,” 325.—E. Dupont. Sur la découverte d’ossements d’Iguanodon,
de poissons et de végétaux dans la-fosse Sainte-Barbe du charbonnage de
Bernissart, 387.—A. Renard. Recherches lithologiques sur les phthanites
du calcaire carbonifére de Belgique, 471.—E. Dupont. Sur les alluvions
torrentielles qui se déposent de nos jours sur les plateaux de l’ Entre-Sambre-
et-Meuse et du Condroz, 643.—C. Malaise. Sur une espéce minérale
- nouvelle pour la Belgique: l’Arsénopyrite ou Mispickel, 881.
: : : Tome xlvu. (1879). - 1879.
C. Malaise. Sur l’Arsénopyrite ou Mispickel et sur l’eau arsénicale de
Court-Saint-Etienne, 29.—P. J. Van Beneden. Sur un enyoi d’ossements
de Cétacés fossiles de Croatie, 183.—C. Malaise. Rapport sur le mémoire
de M. A. Renard: ‘ Des caractéres distinctifs de la dolomite et de la cal-
cite dans les roches calcaires et dolomitiques du calcaire carbonifére de
Belgique,” 492.—A. Renard. Des caractéres distinctifs de la dolomite
et de la calcite dans les roches calcaires et dolomitiques du calcaire car-
bonifére de Belgique, 541.—L. L. de Koninck. Huitiéme et neuviéme
notices sur les minéraux belges, 564 et 568.
: : ? Tome xlviii. (1879). 1879.
Gilkinet. Du développement du régne végétal dans les temps géolo-
giques, 814.
es
250 ADDITIONS TO THE LIBRARY.
Brussels. Académie Royale des Sciences. Bulletins. Série 2.
Tome xlix. (1880). 1880.
Stas. Sur la découverte par le professeur Scacchi, de Naples, d’un
corps simple nouveau dans la lave du Vésuve, 93.—L. G. de Koninck et
Cornet. apports sur le mémoire de M. E. Vanden Broeck “Sur les
phénomenes d’altération des dépots superficiels par V’infiltration des eaux
météoriques, étudiés dans leurs rapports avec la géologie stratigraphique,”
615.—P. J. Van,Beneden. Rapport sur le mémoire de M. G. Cotteau:
“Description des Kchinides tertiaires de Belgique,” 619.
Brussels. Académie Royale des Sciences. Bulletins. Série 2.
Tome |. (1880). 1880.
P. J. Van Beneden. Les Mysticétes & courts fanons des sables des
environs d’Anvers, 11.—L. G. de Koninck. Rapport sur le mémoire de
M. A. Renard “Sur la composition chimique de l’épidote de Quenast,”
80.—A. Renard. Sur la composition chimique de l’épidote de Quenast,
170.—P. J. Van Beneden. Sur deux Plésiosaures du lias inférieur du
Luxembourg, 308.
Mémoires. Tome xliii. 1° Partie. 1880.
A. Briart et F. L. Cornet. Description des fossiles du calcaire grossier
de Mons. 38° partie. Supplément aux deux premiéres parties.
——., ———. Mémoires Couronnés. ‘Tome xxxix, 2° Parnes liso:
: . . Tome xli. 1879.
G. Cotteau. Description des Hchinides du calcaire grossier de Mons.
Tome xlii. 1880.
G. Cotteau. Description des Hchinides tertiaires de la Belgique.
: ‘ . (8vo.) Tome xxix. 1880.
F. V. Rysselberghe. Note sur les oscillations du littoral belge, No. 5.
=) ome nxxex loos
ee ee ee Lome maxon aalioole
Tables des mémoires des membres, des mémoires
couronnés et de ceux des savants étrangers, 1816-57. 1858.
AEE Gee Sg SO:
——. Société Malacologique de Belgique. Annales. Tome xi.
ke iil
C. Paul. Considérations nouvelles sur les systémes Bolderien et
Diestien, 7.—G. Dollfus. Valvata disjuncta, espéce nouvelle des meu-
liéres supérieures des environs de Paris, 27.—-T. Lefévre et A. Watelet.
Additions 4 la faune tertiaire du bassin de Paris. Description de deux
Solens nouveaux, 29.—J. de Cossigny. Tableau des terrains tertiaires
de la France septentrionale, 37. A. Rutot, G. Dollfus et J. Ortlieb.
Rapports sur le mémoire précédente, 40.—T. Davidson. Liste des prin-
cipaux ouvrages, mémoires ou notices qui traitent directement ou indi-
rectement des Brachiopodes vivants et fossiles, 55.—A. Rutot. Quelques
observations relatives aux conclusions de M. Lefévre dans son rapport sur
mon travail intitulé: “ Description de la Rostellaria robusta Rutot,” xi.—
T. Lefévre. Rapport sur le travail de M. Vincent, intitulé: Description
de la faune de l’étage landenien inférieur de la Belgique, xxvii.—J. Deby.
Nécrologie. David Forbes, xxx.—A. Rutot. Rapport sur le travail de
M. G. Vincent, intitulé: Description de la faune de l’étage landenien
inférieur. J¢ partie: Massif du Brabant, xxxvi—H. Vanden Broeck et
ADDITIONS TO THE LIBRARY. 251
Paul Cogels. Observations sur les couches quaternaires et pliocénes
de Merxem prés d’Anvers, Ixviiii—T. Lefévre. Sur la “Note sur la
Rostellaria robusta” par M. Rutot, lxix.
Brussels. Société Malacologique de Belgique. Procés-verbaux des
Séances. Tome vill. 1879.
A. Rutot. Note sur des fossiles du Tongrien inférieur, v.—G. Vincent
et A. Rutot. Observations nouvelles relatives 4 la faune du systéme
Bruxellien et a celle de Vancien Laekenien supérieur, actuellement
systeéme Wemmielien, xii—E. Vanden Broeck et Paul Cogels. Diluvium et
Campinien, réponse a M. C. Dr. Winkler, xviii—A. Rutot. Sur la plus
belle coupe de terrains qui ait jamais été visible aux environs de Bruxelles,
xlvii—k. Vanden Broeck. Compte rendu de l’excursion faite 4 Anvers
les 27 et 28 Juillet 1879, Ixvii.
: : Tome ix. 1880.
P. Cogels et O. Van Ertborn. Nouvelles observations sur les couches
quaternaires et pliocénes de Merxem, v.
: : Tome x. pp. i-xxxvi. 1881.
A. Rutot. Compte rendu d’une course dans le quaternaire de la vallée
de la Somme, aux environs d’Abbeville, vii—A. Rutot. Note sur les
découvertes paléontologiques faites dans ces derniers temps aux environs
d’Erquelennes, xvilii—Stevens. Liste des fossiles recueillis dans les ter-
rains éocénes des environs de Bruxelles, xx.—T. Lefévre. La Rostellaria
ampla, Sol. et ses variétés, xxiv.
Budapest. K. ungarische geologische Anstalt. Jahrbuch. Band iv.
pe bterg 18s.
J. Bockh. Geologische und Wasser-Verhaltnisse der Umgebung der
Stadt Funfkirchen.
Literarische Berichte aus Ungarn. Band iv. Heft 1-4.
1880.
F. Schafarzik. Ueber das Erdbeben in Sud-Ungarn, 642. (For the
continuation of this journal see “ Leipzig. Ungarische Revue.”)
——. Magyar Tudomdnyos Akadémia. Ertekezések a Mathema-
- tikai Tudomdnyok Korébol. Kotet vii. Szdm 3-18. (1879-80).
1879-80.
: . Ertekezések a Természettudomanyok Korébol. Kotet
ix. Szam 20-25. (1879). 1879-80.
G. Stollar. Az Alsé-kekedi gyogyforras chemiai elemzése, Szim 21,
. 3.—L. Solymosi. A Fels6-rakosi savanyuviz valamint a székely-
udvarhelyi hidee sdésfiirdo chemiai elemzése, Sz4m 21, p. 19.—W. A.
Scherfel. A Felsd-ruszbachi asvanyvi? vegyelemzése, Szim 22.—J.
Szabo. A granat és Cordierit (Dichroit) szereplése a magyarorszagi
trachytokban, Szam 25.
: : Kotet x. Szim 1-18 (1880). 1880-81.
T. Ortvay. A magyarorsziei Dunaszigetek foldirati csoportosulésa s
képzodésok tényezoi, Szim 3.—J. Bockh. Adatoka Mecsekhegység és
domboidéke jurakorbeli lerakodasainak ismeretéhez. I. Stratigraphiai
rész. Szam 10.
: . Mathematikai és Termeszettdoményi Kézlemenyek.
Kotet xvi. 1881. :
S. Roth. Szepesmegye nehany barlangjanak leirasa, 618.
252 ADDITIONS TO THE LIBRARY.
Buenos Ayres. Sociedad Cientifica Argentina. Anales. Tomo x.
Entrega 1-6. 1880-81.
J. J.J. Kyle. La Boronatrocalcita de la Provincia de Salta, 169.—
J.J. J. Kyle. Observaciones sobre un depésito fosfatico en la Patagonia,
226.
——. ——. Tomoxi. Entrega 2-5. 1881.
Caen. Société Linnéenne de Normandie. Bulletin. Ser. 3. Vol. i.
(1876-77). 1877.
G.de Tromelin. Etude de la faune du erés silurien dans le Calvados, 5.
—G. Dollfus. Terebripora capillacea: Bryozoaire nouveau du terrain
dévonien du Cotentin, 96.—J. Pépin. Note sur une nouvelle espéce de
Sténéosaure, 115.—L. Crié. Considérations sur la flore tertiaire de Fyé
(Sarthe), 121.—L. Crié. Note sur le Carpolithes Decaisneana, nob., des
erés éocénes de la Sarthe, 123.
: —. : - Vols. 877-78) ome
Moriére. Sur le grés de Bagnoles, 5.—G. de Tromelin. Sur les
terrains paléozoiques de la Basse-Normandie, 6.—Lodin. Note sur le
niveau occupé a Honfleur par Vargile de Kimméridge, 15.—J. Moriére.
Note sur le grés de Bagnoles (Orne), 20.—L. Crié. Note sur les Morinda
de la flore éocéne du Mans et d’Angers, 46.—J. Moriére. Note sur un
tronc fossile paraissant se rapporter au genre Cycadeomyelon, Saporta, 51.
—J. Moriere. Note sur une Astéride fossile nouvelle trouvée dans
Voxfordien des Vaches-noires entre Dives et Villers-sur-Mer, 75.—
Letellier. Deuxiéme excursion de la Société Linnéenne a Alengon, 270.
—Lodin. Du mode de formation et de la classification des terrains supé-
rieurs, 315.—Drouaux. La géologie et l’Exposition géologique au con-
erés du Havre, 525.—Letellier. Note géologique sur les terrains traversés
parle chemin de fer d’Alencgon & Domfront, 340.—Lionnet. Phosphates
de chaux fossiles, géologie et origine, application en agriculture, 351.
Calcutta. Asiatic Society of Bengal. Journal. N.S. Vol. xlvii.
Extra number to Part 1 for 1878. 1880.
: . -——. Vol. xlix. Part 1. Nos. 1—4, and
extra number. 1880-81.
: . Vol. xlx. Part 2. Nos. 1-4. 1880-81.
R. Lydekker. A Sketch of the History of the fossil Vertebrata of
India, 8.
ae
——, ——. ——., Vol.l. Partl. No. fy 133an
~ Volol. Part: 23, Noxieeame Sis
V. Ball. On the Identification of certain Diamond-mines in India,
which were known to and workefl by the Ancients, especially those which
were visited by Tavernier: with a note on the History of the Koh-i-nur,
31.—List of Harthquakes recorded in Assam during the years 1879 and
1880, 61.
. ——. Proceedings. 1880, Nos. 2-10. 1880.
Rey. C. Swynnerton. On a Celt of the Paleolithic Type found at
Thandiani, Punjab, 175.
: 1881, Nos. 1-3. 1881.
V. Ball. On the Identification of certain Diamond-mines in India
which were known to and worked by the Ancients, especially those which
were visited by Tavernier, 2.
ADDITIONS TO THE LIBRARY. 253
Cambridge Philosophical Society. Proceedings. Vol. ui. Parts
ace &-" 18380;
O. Fisher. On the Implement-bearing Loams in Suffolk, 285.—
T. McK. Hughes. On the Transport of fine Mud and Vegetable Matter
by Confervee, 339.—T. M‘K. Hughes. On the Altered Rocks of Anglesea,
341.—W. Keeping. On the included Pebbles of the Neocomian Deposits
of Potton and Upware, and their bearing upon the Physical Features of
the Lower Cretaceous Period, 377.
——. ——. Vol.iv. Part l. 1881.
EH. Tawney and H. Keeping. On the Beds at Headon Hill and Colwell
Bay in the Isle of Wight, 59.
Transactions. Vol. xiii. Part 1. 1881.
Cambridge, U.S.A. Museum of Comparative Zoology at Harvard
College. Annual Report for 1879-80. 1880.
bulketme se Volsvie. Noss oli asso:
——, ——. ——. Vol.vu. No.1. (Geological Series, Vol. i.
Noss) 9 1830-
M. E. Wadsworth. Notes on the Geology of the Iron and Copper
Districts of Lake Superior, 1.
: : Vol. viii. Nos. 1-4. 1880.
C. D. Walcott. The Trilobite: new and old Evidence relating to its
Organization, 192.—H. A. Hagen. The Devonian Insects of New Bruns-
wick, 275.
—_——
: Memoirs. Vol. vi. No.1. 1880.
J.D. Whitney. The Auriferous Gravels of the Sierra Nevada of
California, 289.
: : Wok vm, IN@s 1, ihesl0-
L. Agassiz. Report on the Florida Reefs, 1.
: : ae olen Now. sRartols, 1880.
J.D. Whitney. The Climatic Changes of later Geological Times, 1.
Canterbury. East-Kent Natural-History Society. 12th Report,
1870. Presented by W. Whitaker, Esq., F.GS.
——. ——. 20th Report, 1878. Presented by W. Whitaker,
Esq., F.G.S.
G. Dowker. On Flint Stones, with an account of Banded Flints, 20.—
McDakin. Structure of the Sea-cliffs at Folkestone, 29—M‘Dakin. On
some Fossil Wood from EHastwear Bay near Folkestone, 55.—J. Reid. On
the various Iron-stone Bands in the Strata of Hast Kent, 40.—M*‘Dakin.
On the Tertiaries of the London and Hampshire Basins, 44.
Cardiff Naturalists’ Society. Report and Transactions. Vol. xi.
MOO SoU.
W. J. Sollas. On the Silurian District of Rhymney and Pen-y-lan,
Cardiff, 7—T. Wright. On the Geological Features of the Landscape
seen from Symond’s Yat, 70.
Cassel. Palsontographica. Band xxvii. Lief. 1-6. 1880-81.
Purchased.
F, Romer. Ueber eine Kohlenkalk-Fauna der Westkiiste von Sumatra, 1.
—W. Branco. Beitrige zur Entwickelungsgeschichte der fossilen Cepha-
254 ADDITIONS TO THE LIBRARY.
lopoden, 12.—F’. Sandberger. Ein Beitrag zur Kenntniss der interpleisto-
canen Schichten Englands, 82.—Hans Pohlig. Maritime Unionen, 105.—
M. Neumayr und V. Uhlig. Ueber Ammonitiden aus den Hilsbildungen
Norddeutschlands, 129.
Cassel. Paleeontographica. Supplement iii. Lieferung 8 und 9.
1880. Purchased. |
R. D. M. Verbeek, O. Boettger und K. von Fritsch. Die Tertiar-
formation von Sumatra und ihre Thierreste, 1.
Chemical News. Vol. xli. Nos. 1074. 1880.
. Vol. xlii. Nos. 1075-1101. 1880.
J.A.Church. The Heat of the Comstock Lode, 42,52.—A. C. Ramsay.
Presidential Address to the British Association, 99.—F. A. Massie. On
the Composition of Dufrenite from Rockbridge Co., Va., 181.—F. A.
Massie. Analysis of Amphibole (var. Actinolite) from Amelia Co., Va.,
194.—W. T. Page. Analysis of a Highly Aluminous Pyroxene from
Amhurst Co., Va., 194.—A. L. Baker. Analysis of Ferruginous Mineral,
probably referable to Amphibole, from Amhurst Co., Va., 194.—W. T.
Page. Examination of Livingstonite from a New Mexican Locality, 195.
—W.T. Page. Examination of a altered Livingstonite from Guadalcazar,
S. Luis Potosi, Mexico, 195.—A. Liversidge. Water from a Hot Spring,
New Britain, 324.—A. Liversidge. Water from a Hot Spring, Fiji
Islands, 324.
——. Vol. xl. Nos. 1102-1125. 1881.
H. Leffman. Analyses of some Geyser Deposits, 124.—R. Romanis.
On the Hot Spring at Natmoo near Maulmain, British Burmah, 191.
Chemical Society. Journal. No. 200. 1879.
G. Attwood. Ona Gold Nugget from South America, 427.
: . Nos. 212-217. 1880.
H. Baker. On a Crystal of Diamond, 579.
: . Nos. 218-223. 1881. |
R. H. Davis. The ancient Allum Well at Harrogate, 19.—A. Liver-
sidge. Analyses of Queensland Soils, 61.
es
——
——. Indexes to vols. xxxvii. & xxvii. 1880.
Cincinnati Society of Natural History. Journal. Vol. in. Nos. 2
& 3. 1830.
S. A. Miller. North-American Mesozoic and Czenozoic Geology and
Paleontology, 79.—S. A. Miller. Description of four new species of
Silurian Fossils, 140.—A. G. Wetherby. Remarks on the Trenton Lime-
stone of Kentucky, with descriptions of new fossils from that formation
and the Kaskaskia (Chester) Group, Sub-Carboniferous, 145.—S. A.
Miller. North-American Mesozoic and Ceenozoic Geology and Paleeon-
tology, 165.—S. A. Miller. Descriptions of four new species and a new
variety of Silurian Fossils, and remarks upon others, 282.
Clausthal. Berg- und hiittenminnische Vereins Maja. (Late Natur-
wissenschaftlicher Vereins.) Neue Folge. Heft 2. 1880.
Purchased.
F. Wunderlich. Beitrag zur Kenntniss der Kielschiefer, Adinolen und
Wetzschiefer des nordwestlichen Oberharzes, 1.—H. L. Bridgman. Das
Erzvorkommen im Leadville District, 119.
ADDITIONS TO THE LIBRARY. 255
Copenhagen. Kongelige Danske Videnskabernes Selskab. Natur-
videnskabelige og Mathematiske Afhandlinger. Reekke 5.
Bind xu. No. 6. 1880.
—. ——. ——. Rekke 6. Bindi. Nos. 1&2. 1881.
——. ——. Oversigt. 1880, Nos.2&3. 1889.
1881, No.1. 1881..
Colliery Guardian. Vol. xl. Nos. 1018-1044. 1880,
Hxcursion of the Edinburgh Geological Society to Linlithgow and
Borrowstounness, 95.—The “Lamb-bottom Caves at East Harptree,
Somerset, 186.—British-Association Meeting at Swansea, 346, 375.—
The Coal Industry of the Lower Rhine and of Westphalia, 426,—W.
Saise. The Kurhurballee Coalfields, with some remarks on Indian Coals,
454.—Coal in Cape Colony, 461.—Coal deposits in Natal, 664, 856.—
H. Woodward. The Temperatnre of strata in Coal mines, 903.—W.
Bailes. On Mineral Veins, 1065.
Vol. xli. Nos. 1045-1068. 1881.
John Brown. A description of some borings on the Clifton Estate, and
of the sinking at Clifton Colliery, Nottimgham, 93.—The deepest Coal-pit
in Britain, 387.—The St. Etienne Coalfield, 415.—Coal in Venezueia,
493, 785.
Cracow. Akademija umiejetnosci w Krakowie. Sprawozdanie,
1879. 1880.
Jana Trejdosiewicza. O porfirze w Krélestwie Polsliém, 258.
Darmstadt. Vereins fiir Erdkunde. Notizblatt. 1880. Folge 4.
Heft 1. 1880.
Delémont. Société Jurassienne d’Emulation. L’Emulation Juras-
sienne. 1877, Jan.—Juillet. 1877. Presented by H. B. Wood-
ward, Ksq., F.GS. :
Dorpat. Naturforscher-Gesellschaft. Archiv fiir die Naturkunde.
Ser. 2. Biologische Naturkunde. Band ix. Lief. 1 u. 2.
1880.
— EE
° °
Sitzungsberichte. Band vy. Heft 3, 1880. 1881.
C. Grewinek. Uebersicht der altquartaren und auspestorbenen neu-
quartaren Saug ethiere Liv-, Est- und Kurlands, 339.—C. Grewingk.
Ueber eylindrische Strudel- und Sickergruben in deyonischen Gypslager
bei Diinhof, oberhalb Riga, 359.—M. Ostwald. Ueber Moorseen, 455.—
C. Grewingk. Ueber zwei Geschiebehugel der Westkuste Hstland’s und
deren Entstehungsweise, 439.
Dresden. Naturwissenschaftlichte Gesellschaft Isis. Sitzungs-
berichte. (1880.) 1881. |
Deichmiller. Ueber eine Abhandlung von Walter Keeping “On some
Columnar Sandstone in Saxon Switzerland,” 1—A. Jentzsch. Briefliche
Mittheilungen tiber seme Sammlung sachsischer Diluvialvorkommnisse, 4.
—H.Engelhardt. Ueber den tertiiren Stisswassersandstein von Grasseth, 5.
—E. Zschau. Ueber Mineralvorkommnisse im Granit, 6.—H. B. Geinitz.
Ueber die Fortschritte der geologischen Forschungen in Nordamerika, 59.
—H. Engelhardt. Ueber Pflanzenreste aus den ‘Tertidrablag erungen von
Liehotitz und Putschirn, 77.
‘
256 ADDITIONS TO THE LIBRARY.
Dublin. Royal Geological Society of Ireland. Journal. N.S. Vol. v.
Part 3. 1880.
T. Mellard Reade. A Problem for Irish Geologists in Post-Glacial
Geology, 173.—S. Haughton. Notes on the Annual Water-discharge of
large Rivers, with Indications of some New Methods of Calculation, 177.
—J. P. O'Reilly. On the Occurrence of Microline Feldspar in Dalkey
Granites, 189.—V. Ball. On Spheroidal Jointing in Metamorphic Rocks
in India and elsewhere, producing a Structure resembling Glacial “ Roches
Moutonnées,” 193.—S. Haughton. On Rossetti’s Law of Cooling, applied
to the consideration of the relative effects of Sun-heat, Harth-heat, Star-
heat, and Atmospheric Conditions upon Climates during Geological Time,
199.—G. H. Kinahan. Anniversary Address, 212.—V. Ball. On the
Evidence in favour of the belief in the existence of Floating Ice in India
during the deposition of the Talchir (Permian or Permio-Triassic) Rocks,
223.—V. Ball. On the Coalfields and Coal Production of India, 230.—
V. Ball. On the Mode of Occurrence and Distribution of Gold in India,
258.
——. Royal Irish Academy. . “Cunningham Memoirs.” No. 1.
1880.
——. ——. Transactions. Vol. xxiv. Antiquities. Part 1.
1864.
——. : . Vol. xxvi. Science. Part 22. 1879.
J.P. O'Reilly. Explanatory Notes and Discussion of the Nature of the
Prismatic Forms of a Group of Columnar Basalts, Giant’s Causeway, 641.
: Vol. xxvii. Polite Literature and Antiqui-
ties. Part 3. 1879.
——, Irish Manuscript Series. Vol. 1. Part i
1880.
— . Proceedings. Ser. 2. Vol. i. No. 1, 1869-70.
1870.
W. K. Sullivan. On the Formation of Thenardite in connexion with
the date of the Glacial Period, and the Temperature that prevailed during
it, as deduced from the Influence of the Eccentricity of the Karth’s Orbit
on the Length of Summer and Winter in Aphelion and Perihelion, 2.—
W. K. Sullivan. Note on the Hornblende and Augite Groups of Mine-
rals, 37.
Ser, 2. Vol. i. No. 11, 1874-75. 1875.
pa yf Ce eT Ser) D2) Viol Si NiO egos
ee aan ye eS Oe iolman mmiNoniss ) LSGO,
Eastbourne Natural-History Society. Papers, 1879-80. Presented
by W. Whitaker, Esq., F.G.S. |
A. Ramsay. On the Local, Stratigraphical, and Paleontological Evi-
dence as to the conditions of the Cretaceous Ocean. .
Fast-India Association. Journal. Vol. xii. Nos.1&2. 1880-81.
Easton. American Institute of Mining Engineers. ‘Transactions,
Vol. i. 1871-73. (Philadelphia.) Presented by W. Whitaker,
Esq., F.G.S.
J. F. Blandy. Topography, with especial reference to the Lake Su-
perior Copper District, 75.—J. W. Harden. The Brown Hematite-ore
oe oo
° e
ADDITIONS TO THE LIBRARY. 257
deposits of South Mountain, between Carlisle, Waynesborough, and the
South-eastern Edge of Cumberland Valley, 136.—B. 8. Lyman. On the
Importance of Surveying in Geology, 183.—R. N. Clark. The Tertiary
Coal-beds of Canyon City, Colorado, 293.—T. 8. Hunt. The Geoenos-
tical History of the Metals, 331.—O. J. Heinrich. The Midlothian
Colliery, Virginia, 346.—B. Silliman. On the probable Existence of
microscopic Diamonds, with Zircons and Topaz, in the Sands of Hydraulic
Washings in California, 371.—T. 8. Hunt. Remarks on an Occurrence of
Tin-ore at Winslow, Maine, 372.—T.S. Hunt. The Origin of Metalli-
ferous deposits, 415.
Easton. American Institute of Mining Engineers. Transactions.
Vol. ii. 1873-74. Presented by W. Whitaker, Esq., F.G.S.
T. S. Hunt. The Geology of the North Shore of Lake Superior, 58.—
R. W. Raymond. Remarks on the Occurrence of Anthracite in New
Mexico, 140.—R. W. Raymond. Remarks on the Occurrence of South-
African Diamonds, 143.—R. P. Rothwell. Alabama Coal and Iron, 145.
—T. S. Hunt. The Coals of the Hocking Valley, Ohio, 273.—J. C.
Smock. The Magnetic Iron-ores of New Jersey, their Geographical Dis-
tribution and Geological Occurrence, 514.
: Vol. vi. (1877-78). 1879. Presented by W.
Whitaker, Esq., F.G.S.
A. J. Bowie, jr. Hydraulic Mining in California, 27.—O. J. Heinrich.
The Manhattan Salt Mine at Goderich, Canada, 125.—-C. M. Rolker. The
late operations on the Mariposa Hstate, 145.—J. C. Smock. The Fire
Clays and Associated Plastic Clays, Kaolins, Feldspars, and Fire Sands
of New Jersey, 177.—W.H. C. Hustis. The Nickel Ores of Orford,
Quebec, Canada, 209.—A. L. Holley. Notes on the Iron Ore and An-
thracite Coal of Rhode Island and Massachusetts, 224.—O. J. Heinrich.
The Mesozoic Formation in Virginia, 227.—T. Kgleston. Copper mining
on Lake Superior, 275.—W. 5S. Keyes. The Eureka Lode of Kureka,
Eastern Nevada, 344.—R. W. Raymond. What is a Pipe Vein?, 393,—
J. P. Carson. Iron Manufacture in Mexico, 598.—P. Frazer, jr. Clas-
sification of Coals, 480.—G. H. Cook. On the Southern Limit of the last
Glacial Drift across New Jersey and the adjacent parts of New York and
Pennsylvania, 467.—E. P. Jennings. Analyses of some Tellurium Mine-
rals, 506.—P. Frazer, jr. Missing Ores of Iron, 531.—W. P. Blake. The
Ore-deposits of Hureka District, Hastern Nevada, 554.
Edinburgh. Geological Society. Transactions. Vol. ii. Part 3.
1880.
A. Taylor. On the Crag Structure on the South Slopes of Queen’s
Park, 279.—W. 1. Macadam. On the Chemical Composition of Rocks
from Salisbury Crag (south side), 288.—W. M‘Diarmid. On the North-
east coast of Norfolk, 292.—T. Stock. On a Section recently exposed
near Straiton, 294.—J. Young. On Scottish Carboniferous Microzoa,
999.—H. M. Cadell. On the Volcanic Rocks of the Borrowstounness
Coalfield, 304.—J. Melvin. On the Evidence the Vegetable Soil affords
as to Geological Time, 326.—T. D. Wallace. On the Geology of Rathven
and Enzie, 331.—D’A. W. Thompson. On the Ulodendron and Halonia,
341.—J. Henderson. On some recently discovered Fossiliferous Beds in
the Pentlands, 353.—D. Milne Home. Valedictory Address, 357.
——. Royal Society. Proceedings. Vol. x. 1879-80.
A. Geikie. On the Geology of the Rocky Mountains, 426.—J. Geikie.
The Geology of the Faroe Islands, 495.—J. Murry. On the structure and
VOL. XXXVII. U
258 ADDITIONS TO THE LIBRARY.
origin of Coral Reefs and Islands, 505.—A. Geikie. Rock-weathering, as
illustrated in Edinburgh Churchyards, 518.—Sixth Report of the Boulder
Committee, 577.—R. H. Traquair. Report on Fossil Fishes collected by
the Geological Survey of Scotland in Roxburgshire and Dumfriesshire.
Part I. Ganoidei, 710.—B. N. Peach. On some new Crustacea from the
Cementstone Group of the Calciferous Sandstone Series of Eskdale and
Liddesdale, 711.
Edinburgh. Royal Society. Transactions. Vol. xxix. Part 2.
1880.
Epping Forest and County of Essex Naturalists’ Field Club.
Transactions. Vol.i. Parts 1-3. 1880-81.
H. Walker. A day’s Elephant Hunting in Essex, 27.
Falmouth. Royal Cornwall Polytechnic Society. Forty-eighth
Annual Report. 1880.
Geneva. Société de Physique et d’Histoire Naturelle. Mémoires.
Tome xxvii. Partie 1. 1880.
P. de Loriol. Monographie des Echinides contenus dans les couches
nummulitiques de ’ Egypte, 59.
Geological and Natural-History Repertory and Journal of Prehistoric
Archeology and Ethnology. Edited by S.J. Mackie. 1865-67.
Purchased.
Geological Magazine. Dec. II. Vol. vii. Nos. 7-12. 1880.
W.H. Hudleston. Contributions to the Paleontology of the Yorkshire
Oolites, 289, 391, 481, 529.—T. G. Bonney. Classification of Welsh Pre-
Cambrian Rocks, 298.—R. Etheridge, jun. Contributions to British Tubi-
colar Annelides, 304.—E. Wilson. On the Unconformability of the Keuper
and Bunter, 308.—W. J. M‘Gee. The “ Laterite” of the Indian Penin-
sula, 310.—A. B. Wynne. The Paleozoic Rocks of the Northern Punjab,
313.—T. Davidson. On the Brachiopoda that characterize the Beds of
Brittany and South Devon, 837.—F. Romer. Note on the Genus Cau-
nopora of Phillips, 345.—W. Davies. On the Bones of the Lynx from
Teesdale obtained by Mr. James Backhouse, of York, 546.—J. J. Harris
Teall. Influence of Earth Movements on the Structure of the British
Islands, 349.—J. Croll. Aqueous Vapour in Relation to perpetual Snow,
357.—A.Champernowne. Upper Devonian in Devonshire, 359.—R. Ethe-
ridge, jun. Contributions to a Study of Carboniferous Tubicolar Annelides,
362.—J. G. H. Godfrey. Association of Stibnite and Cinnabar in Mineral
Deposits, 369.—T. M. Reade. Oceans and Continents, 585.—T. G. Bonney.
Pebbles in the Bunter Beds of Staffordshire, 404.—H. H. Howorth. The
Mammoth in Siberia, 408, 491, 550.—W. Keeping. On the Pebbles of
the Upper Neocomian of the South-east of England, 414.—T. Rupert
Jones. Note on a Well lately sunk at Wokingham, 421.—E. T. Newton.
Notes on the Vertebrata of the Pre-Glacial [orest-bed of the East of
England, 424.—C. T. Clough. The “Whin Sill” of Teesdale, as an
Assimilator of the surrounding Beds, 433.—E. T. Newton. Notes on the
Vertebrata of the Pre-Glacial Forest-bed Series of the Kast of Hngland,
447,—E. B. Tawney. Woodwardian Laboratory Notes: North-Wales
Rocks, 452.—Thoroddsen, Thorvald. Volcanic Eruptions and Harth-
quakes in Iceland within Historic Times, 458.—H. Hicks. Pre-Cambrian
Volcanos and Glaciers, 488.—G. R. Vine. On the Carboniferous Polyzoa,
501.—R. J. Ussher. On the Caves and Kitchen-Middens at Carrigagower,
ADDITIONS TO THE LIBRARY. 259
Co. Cork, 512.—T. G. Bonney. On some Serpentines from the Rheetian
Alps, 538.—R. B. Foote. Notes on the Occurrence of Stone Implements
in the Coast Laterite south of Madras, 542.—A. Liversidge. Analyses of
Moa Eege-shell, 546.—C. Reid. Classification of the Pliocene and Pleis-
tocene Beds, 548.
Geological Magazine. N.S. Dec. IL. Vol. viii. Nos. 1-6. 1881.
T. Dayidson. On Spiral-bearing Brachiopoda from the Wenlock and
Ludlow Shales of Shropshire, 1—H.G. Seeley. Ontwo Ornithosaurians
from the Upper Greensand of Cambridge, 18.—O. Fisher. Oblique and
Orthogonal Sections of a folded Plane, 20.—F. D. Longe. On the Oolitic
Polyzoa, 23.—R. H. Traquair. On New Fish-remains from the Blackhand
Ironstone of Borough-Lee, near Edinburgh, 34.—W. H. Hudleston. Contri-
butions to the Paleeontology of the Yorkshire Oolites, 49, 110.—J. D. Dana.
Metamorphism of Massive Crystalline Rocks, 59, 110, 162.—B. N. Peach
and J. Horne. The Glaciation of the Shetland Isles, 65.—J. Smith and
T. Rupert Jones. Upper Silurian Entomostraca, 70.—T. Mellard Reade.
Oceanic Islands, 75.—T. Stock. On anearly entire Rhizodus at Wardie,
77.—W. J. Sollas. On Striated Triassic Pebbles, 79.—A. B. Wynne.
On the Travelled Blocks of the Upper Punjab and a supposed Glacial
Period in India, 97.—T. Davidson and George Maw. On the U. Silu-
rian Rocks of Shropshire, with their Brachiopoda, 100.—W. A. E.
Ussher. Pre-historic Europe and the Cornish Forest-beds, 151.—G. H.
Kinahan. ‘ Laccolites, 134.—T. Davidson. New Upper Silurian Bra-
chiopoda from Shropshire, 145—G. M. Dawson. Geology of British
Columbia, 156, 214.—W. H. Herries. Woodwardian Laboratory Notes:
Part 5. The Bagshot Beds, 171.—G. W. Lamplugh. Ona Shell-bed under
the Drift at Speeton near Filey, Yorkshire, 174.—T. Rupert Jones. On the
Carboniferous System in Britain, 181.—H. Woodward. Note on a Head-
shield of Zenaspis Salwey?, 193.—R. D. Roberts. Position of the Twt-Hill
Conglomerate, 194.—T. Mellard Reade. AXjolian Sandstone, 197.—H. H.
Howorth. The Mammoth in Europe, 198, 251.—D. Milne Home. Glaci-
ation of the Shetlands, 205.—W. G. Lock. _ Volcanic History of Iceland,
212.—J. S. Gardner. Subsidence and Elevation, 241.—J. H. Marr.
Classification of the Cambrian and Silurian Rocks, 245.—K. 'T. Newton.
The Vertebrata of the Forest-bed Series of the East of England, 256.—
C. Lapworth. Correlation of the Lower Paleozoic Rocks of Britain and
Scandinavia, 260.
eV Olivia NOS (oe LOoOn weeunchascd.
VO) Vili NOSa lO.) el GOlionn eeeneRased.
Geologists’ Association. Proceedings. Vol. vi. Nos. 7-9. 1880
and 1881.
Visit to the Museum of Practical Geology, Jermyn Street: Demon-
stration on the Minerals in the Horse-shoe Case; reported by W. H.
Hudleston, 311.—J. S. Gardner. Excursion to the Hampshire Coast,
316.—R. Owen. Visit to the British Museum: Demonstration on the
Elephantine Mammals, 321.—T. Rupert Jones, A. Irving, and C. Cooper
King. Excursion to Camberley, 529.—W. Whitaker. Excursion to
Upnor, 336.—W. H. Hudleston. Excursion to Oxford.—W. H. Hudle-
ston. Excursion to Aylesbury, 344.—A. Taylor. On the Origin and
Petrology (specially of the South side) of Salisbury Crags, Edinburgh,
303.—J. W. Davis. On the Fish Fauna of the Yorkshire Coal-tield, 359.
—Excursion to Kew Gardens, Richmond, and Kineston Hill, 370.—Ex-
eursion to Croydon and Riddlesdown, 372.—Excursion to Redhill, 373.
u 2
260 ADDITIONS TO THE LIBRARY.
W. J. Sollas. On the Geology of the Bristol District, 375.—Excursion
to Maidstone, 392.—Excursion to Leith Hill and Dorking, 393.—Excur-
sion to Bristol, 396.—G. 8. Boulger. On the Geological and other
Causes that Affect the Distribution of the British Flora, 403.—J. F.
Blake. On the Classification of Rocks, 418.—EH. Renevier. A Petro-
graphical Classification of Rocks, 426.—T. Rupert Jones. Onthe Geology
and Physical Features of the Bagshot District, 429.
Geologists’ Association. Proceedings. Vol. vii. No.1. 1881.
_ T. Rupert Jones. Presidential Address, 1—H. Hicks. On some
Recent Researches among Pre-Cambrian Rocks in the British Isles, 59.
Giessen. Oberhessische Gesellschaft fiir Natur- und MHeilkunde.
Neunzehnter Bericht. 1880.
A. Nies. Vorlaufiger Bericht tiber zwei neue Mineralien von Grube
Eleonore am Diinsbere bei Giessen, 111.—A. Streng. Ueber die Phosphate
von Waldgirmes, 151.
Gloucester. Cotteswold Naturalists’ Field Club. Proceedings.
1879-80. i880.
Sir W. V. Guise, Bart. Presidential Address, 1879, 94.—K. Witchell.
On a Section of Stroud Hill and the Upper Ragstone Beds of the Cottes-
wolds, 118.—Sir W. V. Guise, Bart. Presidential Address, 1880, 157.—
T. Wright. On the Modern Classification of the Ammonitide, 170.
Haarlem. Société Hollandaise des Sciences. Archives Néerlandaises
des Sciences Exactes et Naturelles. Tome xv. Livr. 3-5.
1880.
Halifax, N.S. Nova-Scotian Institute of Natural Science. Pro-
ceedings and Transactions. Vol. v. Part 2. 1880.
D. Honeyman. Nova-Scotian Geology, Annapolis County, 119.—D.
Honeyman. Geological Waifs from Mag dalen Islands, 1836,—D. Honey-
man. Nova-Scotian Geology : Notes on a New Geological Progress Map
of Pictou County, 192.
Havre. Socicté Géologique de Normandie. Bulletin. Tome v.
1878. (1880 ?)
G. Lionnet. Réunion de la Société Linnéenne de Normandie a Alen-
gon les 15 et 16 Juin 1878 (premiere journée), 40.—G. Drouaux. Réunion
de la Société Linnéenne de Normandie a Alencon les 15 et 16 juin 1878
(deuxiéme journée), 53.—G. Drouaux. La Géologie et ’ Exposition gé0-
logique au Congrés du Havre, 74.—H. Savalle. Note sur les sables néo-
comiens de la Héve et sur quelques espéces f fossiles qui y ont été recueil-
lies, 94.—E Savalle. Note sur une espéce de crustacé fossile trouvé dans
les sables micacés de la Héve, 98.—H. Savalle. Note sur les sables mi-
cacés de la Héve, 100.—F. Prudhomme. Rapport sur le Tome V. des
Annales de la Société Géologique du Nord, 106.—C. Brylinski. Note
sur l’Hozoon canadense, 114.—M. Gourdon. Note sur quelques blocs
erratiques de la Vallée de Valencia de Arreu, Catalogne, 119.—(G. Lion-
net’). Notes sur quelques substances minérales servant aux Arts ou a
VIndustrie, 120.—G. Biochet. Note sur le dolmen troué d’Aizier, Kure,
137.
; Tome vi. 1879. 1880. (Exposition Géo-
logique et Paléontologique du Havre en 1877.)
Description de l’ixposition, 1—G. Lennier et G. Lionnet. Résumé
sur la Géologie Normande, 29.—Letellier. Les terrains des environs
ADDITIONS TO THE LIBRARY. 261
d’Alencon, 525.—W. A. E. Ussher. Etude sur les roches triasiques de
Normandie et sur les dépdts limitrophes, 531.—A. Durand. L’étage co-
rallien sur le littoral du Calvados, 563.—E. Savalle. Note sur les sables
micacés de l’étage néocomien, ala Héve, et sur quelques espéces fossiles
découvertes récemment a ce niveau, 577.—G. Dollfus. Essai sur l’ex-
tension des terrains tertiaires dans le bassin anglo-parisien, 584.—G.
Cotteau. Catalogue des Kchinides jurassiques de Normandie, 606.—G.
de Saporta. Notice sur les végétaux fossiles de la craie inférieure des
environs du Havre, 640.—G. Drouaux. Combustibles minéraux en Nor-
mandie, 662.—C. Marchand. De la composition chimique des calcaires
exposés par la Société Géologique de Normandie, 692.—Besnou. Consi-
dérations sommaires sur quelques produits sousmarins, et analyses de ces
produits, 704.—E. Marchand. Considérations générales sur la constitu-
tion des eaux potables et en particulier des eaux du terrain crétacé dans
les arrondissements du Havre et d’Yvetot, 742.—H. Meurdra. Etude
sur le regime des sources du Havre, 777.—E. T. Hamy. Notes d’an-
thropologie paléontologique, prises a l’Exposition du Havre, 791.—D.
Bourdet. L’archéologie préhistorique 4 l’Exposition du Havre, 807.—C.
Beaugrand. Note sur quelques silex taillés des environs d’Yvetot et du
Havre, 846.
Heidelberg. Naturhistorisch-medicinischer Verein. Verhandlungen.
Neue Folge. Bandii. Heft 5. 1880.
A. Schmidt. Die Zinkerz-Lagerstitten von Wiesloch, Baden, 369.
Institution of Civil Engineers. Minutes of Proceedings. Vol. lx.
1880.
: Nola eS ssv:
J. Lucas. The Hydrogeology of the Lower Greensands of Surrey and
Hampshire, 200.—G. Attwood. The Chile Vein Gold Works, South
America, 244,
Vol. lxu. 1880.
——. ——. Vol. lxii. 188].
Kansas. Kansas City Review of Science and Industry. Vol. i.
No. 10. 1879. Presented by W. Whitaker, Esq., F.G.S.
: Vol. 1. No. 6. 1879.
B. F. Mudge. Botany and Evolution, 321.—E. P. West. Following
the Pick and the Spade, 328.—W. H. R. Lykins. The Stone Age in
Kansas, 331.
: Vol. 11. No. 9. 1880.
J. A. Smith. Some Objections to Mcdern Geological Teachings, 740.
—The Attractions of the Yellowstone National Park, 745.
: oP Voleiv= No: I 7kS80:
T. M‘K. Hughes. Antiquity of Man Questioned, 19.
Lausanne. Société Vaudoise des Sciences Naturelles. Bulletin.
Sér. 2. Tome xvii. No. 84 1880.
E. Schmidt. Analyse de Veau de Vernex-dessus, 15.—G. Maillard.
Nouveau gisement de feuilles fossiles, 32.—P. de la Harpe. Note sur les
Nummulites Partschi and Oosteri, de la H., du calcaire du Michelsberg,
pres Stockerau (Autriche) et du Gurnigelsandstein de Suisse, 33.—G.
Maillard. Notice sur la molasse dans la ravine de la Pandéze au Moulin
de Belmont, 81.—W. Fraisse. Note sur les érosions de Vallamand, 157.
262 ADDITIONS TO THE LIBRARY.
Leeds. Philosophical and Literary Society. The Annual Report
for 1879-80. 1880. 3
——. Yorkshire Geological and Polytechnic Society. Proceedings.
Vol. vu. Part 3, 1880. 1881.
J. W. Davis. On the Distribution of Fossil Fish in the Yorkshire
Coal-fields, 228.—G. W. Lamplugh. Ona Faultin the Chalk of Flambro’
Head, with some Notes on the Drift of the Locality, 242._J. R. Dakyns.
On Glacial Deposits North of Bridlington, 246.—J. Magens Mello. Ona
Short History of the Creswell Caves, 252.—J. W. Davis. On a Group
of Erratic Boulders at Norber, near Clapham, in Yorkshire, 266.—W. H.
Wood. Ona Chemical Method of Distinguishing Black Obsidian from
Black Blast Furnace Slag, 274.—W. Y. Veitch. On the Geology of the
District around Middlesborough, 284.—T. Allison. Notes on the Geology
of the Cleveland District, 285.—L. C. Miall. On some Bones of Ctenodus,
289.—J. W. Davis. Report of the Raygill Fissure Exploration Commit-
tee, 800.—J. W. Davis. Summary of Geological Literature relating to
Yorkshire, published during 1878, 1879, and 1880, 319.
Leipzig. Naturforschende Gesellschaft. Sitzungsberichte. Jahr-
gane vi. 1879. 1880.
: : . Jahrgang vi. 1880. 1881.
H. Credner. Ueber die geologischen Resultate einer Tiefbohrung am
Berliner Bahnhofe zu Leipzig, 1.
——, Ungarische Revue. 1881. Hefte 1-3. 1881.
——. AZeitschrift fiir Krystallographie und Mineralogie. (Groth.)
Band iv. Hefte5&6. 1880. Purchased.
H. Laspeyres. Mineralogische Bemerkungen,433.—L. Calderon. Ueber
die optischen Eigenschaften der Zinkblende von Santander, 504.
(——.) Band v. Hefte 1-6. 1880-81. Pur-
chased.
G. vom Rath. Mineralogische Mittheilungen, 1—A. Damour und G.
vom Rath. Ueber den Kentrolith, eine neue Mineralspecies, 32.—A.
Bertin. Ueber eie Farben von Krystallplatten im elliptisch polarisirten
Lichte, 36.—V. von Zepharovich. Mineralogische Notizen, 96.—A. Brun.
Mineralogische Notizen, 103.—W. Voigt. Ueber den Einfluss einer
Kriummung der Prismenflachen auf die Messungen von Brechungsindices
und tiber die Beobachtungen des Herrn Calderon an der Zinkblende, 113.
—W.Websky. Ueber die Berechnung der Elemente einer monoklinischen
Krystallgattung, 168,—G. J. Brush und E. 8. Dana. Ueber Krystalli-
sirten Danburit von Russell, St. Lawrence County, New York, 183.—G.
J. Brush und E. 8. Dana. Ueber die Mineralfundstatte von Branchville,
Connecticut: der Spodumen und seine Zersetzungsprodukte, 191.—A.
Grosse-Bohle. Ueber das optische Verhalten des Senarmontils und der
reguliren arsenigen Saure, 222.—A. Damour und G. vom Rath. Ueber
den Trippkeit, eme neue Mineralspecies, 245.—M. Guyot. Ueber einen
ungewohnlich grossen Huklaskrystall, 250.—F. Sansoni. Hin neues Vor-
kommen von krystallisirten Manganspath, 250.—F. Sansoni. Pyrit vom
Binnenthal, 252.—P. Groth. Beitrag zur krystallographischen Kenntniss
des Wismuthglanzes, 252.—P. Groth. Hine Pseudomorphose aus dem
Binnenthal, 253.—G. vom Rath. Mineralien von Zoptau, 253; Baryt
in Basalt, 256; Mineralien von Copiapo in Chile, 256; Ueber Fahlerz
von Horhausen, 258; Diaspro vom Greiner, 259.—D. M. Kramberger.
Pilarit, ein neues Mineral aus der Gruppe des Chrysocolla, 260.—C. Délter.
ADDITIONS TO THE LIBRARY. 263
Krystallographisch-chemische Studien am Vesuvian, 289,—G. A. Konig.
‘ Jarosit von einer neuen Fundstatte, 317.—G. A. Konig. Beegerit, ein
neues Mineral, 322.—A. von Lasaulx. Mineralogische Notizen, 326.—H.
Forstner. Cossyrit, ein Mineral aus den Liparitlaven der Insel Pantel-
laria, 348.—H. Forstner. Ueber kunstlichen Wurtzit, 363.—C. Vrba.
Mineralogische Notizen, 417.—J. Beckenkamp. Ueber die Ausdehnung
monosymmetrischer und asymmetrischer Kvystalle durch die Warme, 436.
—G. J. Brush. Ueber amerikanische Sulfoselenide des Quecksilbers, 467.
—A. Arzruni und 8. Koch. Ueber den Analcim, 483.—G. vom Rath.
Quarz und Feldspathe von Dissentis, 490.—G. vom Rath. Lamellare
Zwillingsverwachsung des Augit nach der Basis, 495.—P. Groth. Hinige
Erwerbungen der Strassburger Universitatssammlung, 496.—J. Lehmann.
Krystallographische Mittheilungen,529.-M. Websky. Ueber Descloizit
und Vanadinit aus La Plata, 542.—H. Bamberger und K. Feussner. So-
dalith von Tiahuanaco, 580.
Lille. Société Géologique du Nord. Annales. Tome yii.(1879-80).
1881.
Ladriére. Documents nouveaux pour l'étude du terrain dévonien des
environs de Bavai, 1—Ladriére. Le terrain quaternaire du Nord, 11.—
A. Rutot et EH. Vanden Broeck. Les phénomenes post-tertiaires en Bel-
gique dans leurs rapports avec Vorigine des dépdts quaternaires et
modernes, 33.—A. Potier. Lettre a M. Gosselet au sujet de l’argile a
silex, 53.—Ortlieb. Compte-rendu d’une excursion géologique a Renaix,
Belgique, 67.—De Lapparent. Note sur l’argile 4 silex du Nord de la
France, 79.C. Barrois. Note sur les alluvions de la Serre, Aisne, 82.
—A. Rutot. Note sur une coupe de terrain observée dans la Gare de
Frameries prés Mons, Belgique, 92.—Gosselet. Notes sur les sables ter-
tiaires du plateau de l’Ardenne, 100.—Potier. Resultats de deux sondages
de Sangatte, 112.—F. Romer. Le genre Oldhama, Forbes, 115.—
Gosselet. De Vusage du droit de priorité et de son application aux noms
de quelques Spiriféres, 122.—Gosselet. Roches cristallines des Ardennes,
132.—C. Barrois. Sur les recherches géologiques de Mr. G. K. Gilbert
dans les monts Henry, 160.—Gosselet. Division a établir dans le terrain
diluvien de la vallée de la Somme, 165.—C. Barrois. Note sur l’étage
turonien de l’Irlande, 175.—C. Barrois. Note sur la fauna quaternaire
de Sangatte, 181.—Ladriére. Observations sur le terrain crétacé des envi-
rons de Bavai, 184.—Gosselet. Sondage de Menin, 188.—Van Ertborn.
Sur la position du Diestien, et lage des sables blancs de Herenthals, 191.—
J. Ortlieb. Lettre a M. le Maire de Tourcoing au sujet de 1’établisse-
ment d’un Cimetiére, 192.—Gosselet. Troisiéme note sur le Famennien:
tranchée du chemin de fer du Luxembourg; les schistes de Barvaux, 195.
—Jannel. Note sur la présence de phosphates dans le lias des Ardennes
et de la Meuse, 201.—Gosselet. Quatriéme note sur le Famennien:
divisions a établir dans les schistes et les Psammites des environs de
Maubeuge, 206.—Ladriére. Note sur les tranchées des chemin de fer
d’Henin-Lietard a Carvin, 211.—P. Hallez. Discours présidentiel, 217.
—T. Barrois. Rapport sur les travaux de la Société en 1878-79, 229.—
Gosselet. Compte-rendu de l’excursion aux environs de Saint-Omer, 235.
—N.de Mercey. Note sur la confusion résultant de l’emploi de la déno-
mination d’argile a silex appliquée a deux dépéts placés, l’un a la base,
et autre au sommet de la série tertiaire du Nord de la France, 237.—_N.
de Mercey. Observations a occasion de quelques travaux publiés dans
les Annales de la Société géologique du Nord sur le quaternaire ancien,
246.—C. Barrois. Sur le terrain silurien supérieur de la presqwile de
Crozon, 258.—Gosselet. Description géologique du canton de Berlaimont,
270.—J. Ladriére. Etude sur les limons des environs de Bavai, 302.—
264 ADDITIONS TO THE LIBRARY.
P. Duponchelle. Compte-rendu de l’excursion du 29 aott au 7 sep-
tembre 1879 dans les terrains primaires de l’Ardenne et de |’Hifel, 319.
—C. Maurice. Compte-rendu de lexcursion du 3 au 7 septembre 1879
dans les régions volcaniques de |’Hifel, 331.—C. Maurice. Compte-rendu
de l’excursion géologique du 29 mars au 1° avril 1880 dans le Boulon-
nais, 300.—P. Duponchelle. Gris-Nez et environs de Marquise, 360.—
J. Coroénne. Compte-rendu de l’excursion du jeudi 29 avril 1880 4
Sainghin, 369.—C. Maurice. Compte-rendu de l’excursion du 2 mai
1880, 572.—J. Coroénne. Compte-rendu de l’excursion du 6 juin 1880,
a Ath et a Lens, 376.—Trachet. Compte-rendu de excursion géologique
du i6 au 18 mai 1880, dans V’arrondissement d’Avesnes, 379.
Linnean Society. Journal. Zoology. Vol. xv. No. 82. 1880.
. Nos. 83-85. 1880-81.
EH. Ray Lankester. On the Tusks of the fossil Walrus found in the
Red Crag of Suffolk, 144.—P. H. Carpenter. On the Genus Solanocrinus,
Goldfuss, and its Relations to recent Comatule, 187.
Botany. Vol. xvii. Nos. 106-112. 1880-81.
——. Transactions. 2nd Ser. Botany. Vol. i. Parts 8 & 9.
1880.
Lisbon. Academia Real das Sciencias. Jornal de Sciencias Mathe-
maticas, Physicas e Naturaes. Vol. vi. No. 24. 1878.
, : Vol. vii. Nos. 25-28. 1879-80.
J.F.N. Delgado. Correspondance relative a la classification des schistes
siluriens a Néreites découverts dans le sud du Portugal, 103.—J. C. B.
Cotter. Fosseis das bacias terciarias marinas do Tejo, do Sado e do
Algarve, 112.
——_., —_—_——-=-,
Vol. viii. No. 29. 1880.
——, —-—. Sessdo publica em 9 de Junho de 1880. 1880.
: Memorias. Classe de Sciencias Mathematicas, Phy-
sicas e Naturaes. Ser. 2. Tomov. Parte 2. 1878.
J. Filippe Nery Delgado. ‘Terrenos paleozoicos de Portugal, sobre a
existencia do terreno siluriano no Caixo Alemtejo.— Carlos Ribeiro.
Estudios prehistoricos em Portugal. Noticia d’algumas estacoes e monu-
mentos prehistoricos. Noticia da estagao humana de Licéa.
. Sociedade de Geographia. Boletin. Ser. 2. Nos. 1-4.
1880-81.
Liverpool. Geological Society. Proceedings. Session 21st (1879-80).
Vol. iv. Part 2. 1880.
W.Semmons. Presidential Address, 98.—C. Ricketts. On the Car-
boniferous Limestone near Skipton and in North Derbyshire, 132-—T,
M. Reade. The Glacial Beds of the Clyde and Forth, 159.—R. A. Esk-
rigge. Notes on human Skeletons and Traces of human Workmanship
found in a Cave at Llandudno, 153.—W. Boyd Dawkins. Memorandum
on the Remains found in the same Cave, 156.
. Naturalists’ Field Club. Proceedings for the year 1879-80.
1880. Presented by W. Whitaker, Esq., F.GS.
London, Edinburgh, and Dublin Philosophical Magazine. Series 5.
Vol. x. Nos. 59-64. 1880. Presented by Dr. Francis, F.L.S.,
———
ADDITIONS TO THE LIBRARY. 265
London, Edinburgh, and Dublin Philosophical Magazine. Series 5.
Vol. xi. Nos. 65-71. 1881. Presented by Dr. Francis, F.GS.
London. Hertfordshire Natural-History Society and Field Club.
Transactions. Vol.i. Part1l. 1880.
J. E. Harting. Animals which have become extinct in Britain within
historic times, 5.
London Iron-Trades Exchange. Vol. xxvi. No. 1098. 1880.
. Vol. xxvii. Nos. 1099-1124. 1880.
The Minerals of New South Wales, 7, 66, 134, 169, 196, 237, 268.
Vol. xxviii. Nos. 1125-1199.. 1881.
Petroleum in Venezuela, 397.—Extinct Monsters in a Coal Mine, 536.
Manchester. Geological Society. Transactions. Vol.xv. Parts 14—-
18. 1880.
J.B. Perrin and John Plant. On coucretionary Nodules of Limestone
and foliated Mouldings in the Permian Marls near Leigh, 305.—W. Watts.
Geological Strata, and Mode of Procedure in driving a Tunnel at Saddle-
worth, 352.—J. D. Kendall. The Formation of Rock-basins, 368.—C. HE.
De Rance. Further Notes of Triassic Borings near Warrington, 388.
4 Vol. xvi. Parts 1-5. 1881.
J. Dickinson. On the Discovery of Rock-Salt at Preesal, Lancashire
26.—H. A. Woodward. On the Temperature of Strata and Seams of
Coal taken in the new Sinkings of the Clifton and Kersley Coal Company
at Newtown Collieries, Clifton, 29.—G. Wild. On marine fossil Shells
at Ashton Moss Colliery Sinking, near Ashton-under-Lyne, 37.—W.
Watts. On “ Arctic Peat Bog,” Rhodes Bank, Oldham, 43.—G. H. Kina-
han. Jron-masked Rocks, 77.—J.T. Boot. Sections of Collieries and
Bore-holes, 83.
——. Literary and Philosophical Society. Memoirs. Series 3.
Wolk vi. £379.
Rooke Pennington. A Descent into Elden Hole, Derbyshire, 1.—A.
W. Waters. Inquiries concerning a Change in the Position of the Earth’s
Axis, 110.—C. A. Burghardt. On the Origin of some Ores of Copper, 171,
253.—E. W. Binney. Notice of a fossil Plant found at Laxey, in the
Isle of Man, 214.—J. B. Hannay. On Siliceous Fossilization, 234.
. Proceedings. Vol. xvi. (1876-77). 1877.
W. Boyd Dawkins. Address, 34.—J. Plant. Wealden Fossils from
Columbia, 8. America, 50.—M. Stirrup. The Raised Beaches of the
County Antrim, their Molluscan Fauna and Flint Implements, 51.—M,
M. Pattison Muir. Note on a Manganese Ore from New South Wales,
and on a Specimen of native Silver from New Zealand, 58.—H. Grim-
shaw. On a Mineral Water from Humphrey Head, near Grange Sands,
North Lancashire, 63.—E.W. Binney. A Notice of some organic Remains
from the Schists of the Isle of Man, 102.—A. W. Waters. Inquiries
concerning a Change of Position of the Earth’s Axis, 171.—John Plant.
Footprints of Dinornis, Bones of Dinornis and Dodo, 181.—M. Stirrup.
Upon Specimens from the Fresh Water Deposits of La Limagne d’Auvergne
in Central France, 182.—E. W. Binney. Note on the Upper Coal-Measures
of Canobie, Dumfriesshire, 192.
——. ——. ——. Vol. xvii.(1877-78). 1878.
A. W. Waters. Table of Effect of Movements of the Surface of the
Globe on the Shifting of the Axis of the Earth, 2.—E. W. Binney. On
266 ADDITIONS TO THE LIBRARY.
some Coal-Measure Plants and other organic Remains from Spain, 5.—
M. M. Pattison Muir. Note on an Edible Clay from New Zealand, 6. —
C. A. Burghardt. On the Origin of some Ores of Copper, 27, 151.—E.
W. Binney. Notice of a large Boulder Stone at Old Trafford, Manchester,
54.—W. C. Williamson. On the Microscopic Conditions of a Slab from
the Mountain Limestone of Bolland, 70.—K. W. Binney. Notice of a
fossil Plant found at Laxey, in the Isle of Man, 85.—J. B. Hannay. On
Siliceous Fossilization (Part 1), 97.
Manchester. Literary and Philosophical Society. Proceedings.
Vol. xvi. (1878-79). 1879.
HK. W. Binney. On Boulders of Clay from the Drift, 40.—C. Grimshaw
and H. Grimshaw. Ona further Analysis of the Water of the Mineral
Spring at Humphrey Head, 45.—A. Bell. The Area of the Middle Drifts
as determined by their Contents, 51.—J. B. Hannay. On Siliceous Fos-
silization (Part 2), 75.—C. A. Burghardt. Mineralogical Notes, 111.—
EK. W. Binney. On the Marine Shells found in the Lancashire Coalfields,
117.
——, ——. ——. Vol. xix. (1879-80). 1880.
i. W. Binney. Notes on some Fossils from the Iron Mines of Furness,
5.—J. Plant. Bog-butter (Butyrellite), from Co. Galway, Ireland, 70,—
EK. W. Binney. Notes on a Bore through Triassic and Permian Strata
lately made at Openshaw, 98.—J. Plant. On Flexible Sandstone, 103.—
J. Plant. On the Use of Infusorial Earth, 106.—Watson Smith. The
Castel Nuovo Lignite Deposit, near San Giovanni, Tuscany, 135.
Melbourne. Royal Society of Victoria. Transactions and Proceed-
mares) Wolk cyly Were
A. W. Howitt. The Diorites and Granites of Swift’s Creek and their
Contact Zones, with Notes on the Auriferous Deposits, 11.—J. Cosmo
Newbery. Some new Localities for Minerals in Victoria, 144.—N. Taylor.
Notes on the Geology of the West Tamar District, Tasmania, 155.
Middlesbrough. Cleveland Institution of Engineers. Proceedings,
1879-80. No.6. Presented by G. Barrow, Esq., F.GS.
G. Barrow. On the Cleveland Ironstone (Part 2), 180.
Mineralogical Society. Journal. Vol.iv. Nos. 17-19. 1880-81.
J. H. Collins. On some Cornish Tin-stones and Tin-capels, 1, 103.—
Heddle. The Geognosy and Mineralogy of Scotland, County of Caith-
ness, 21.—J. P. Howley. List of Newfoundland Minerals, 36.—A. French.
On a peculiar pasty Form of Silica from a Cavity in Gold-bearing Quartz,
42.—Heddle. On anew Face on Crystals of Stilbite from two Localities,
43.—T. A. Redwin. Further Notes on Mineral Growth, 96.—Heddle.
Preliminary Notice of Substances which may prove to be new Minerals,
117.—W. Terrill. On certain crystallized Products formed in Smelting
Operations, 133.—Heddle. On the Geognosy and Mineralogy of Scotland :
Sutherland, 185.—H. C. Bolton. Action of Organic Acids on Minerals,
181.—Heddle. On Substances which may prove to be new Minerals, 189.
—C.0O.Trechmann. On crystallized Olivine from Slag, 192.
Montreal. Canadian Naturalist. N.S. Vol.ix. Nos. 6-8. 1880-81.
J. W. Dawson. New Facts respecting the geological Relations and
fossil Remains of the Silurian Ores of Pictou, Nova Scotia, 352.—G. F.
Matthew. ‘Tidal Erosion in the Bay of Fundy, 368.—T. Sterry Hunt.
Geological Notes, or Abstracts of recent Papers, 429.—C. U. Shepard.
A peculiar Mineral of the Scapolite Family, 437.—J. W. Dawson.
Revision of the Land Snails of the Paleozoic Era, with Descriptions of
ADDITIONS 'TO THE LIBRARY. 267
new Species, 449.—F. Bain. Note on Fossils from the Red-Sandstone
System of Prince-Edward Island, 463.
Montreal. Canadian Naturalist. N.S. Vol. x. No.1. 1881.
J. W. Dawson. Paleontological Notes, 1—A. W. Wright. On the
gence Substances contained in the Smoky Quartz of Br anchv ille, Conn.,
2.—G. M. Dawson. Note on the Geology ‘of the Peace-River Recion, 20.
YS F, Whiteaves. Ona new Species of Ptertchthys, allied to Bothrio-
lepis ornata, Kichwald, from the Devonian Rocks of the north side of the
Baie des Chaleurs, 25. a F’, Whiteaves. Description of a new Species
of Psammodus from the Carboniferous Rocks of the Island of Cape
Breton, 36.—R. Chalmers. On the Glacial Phenomena of the Bay-
Chaleur Region, 37.—C. Hoffmann. Recent Analyses of Canadian
Minerals and River-waters, 55.
Montrose. Natural-History and Antiquarian Society. Report of
the Directors, 1881. 1881. Presented by W.S. Dallas, Esq.,
FLS. | |
R. Barclay. Mineralogy of the Arbroath and Montrose Railway-cut-
ting, 8.
Moscow. Société Impériale des Naturalistes. Bulletin. Tome liv.
(1879). No.4. 1880.
Tome lv. Nos. 1 & 2. 1880.
V. Kiprijanoff. Ueber fossile Fische des Moscauer Gouvernements, 1.
—W. H. Twelvetrees. On a Labyrinthodont Skull (Platyops Rickardi,
Twelvetr.) from the Upper Permian Cupriferous Strata of Kargalinsk
near Orenbure, 117.—W. H. Twelvetrees. On Theriodont Humeri from
the Upper Permian Copper-bearing Sandstones of Kargalinsk near Oren-
burg, 123.—H. Trautschold. Zur Frage uber das Sinken des Meeres-
spiegels, 174.
Munich. K6niglich-bayerische Akademie der Wissenschaften. Ab-
handlungen der mathematisch-physikalischen Classe. Band xii.
Abth. 3. 1880.
. Sitzungsberichte der mathematisch-physikalischen
Classe. 1879, Hett 4. 1879.
. 1880, Hefte 1-4. 1880.
C. W. Giimbel. Geognostische Mittheilungen aus den Alpen, 164,
542.—C. W. Giimbel. Ueber die mit einer Flissigkeit erfullten Chalce-
donmandeln (Enhydros) von Uruguay, 241.—F. Pfaff. Petrographische
Untersuchungen iiber die eocenen Thonschiefer der Glarner Alpen, 461.
‘ . ——. 1881, Hefte lund 2. 1881.
V. Kobell. Ueber Polarisationsbilder an Zwillingen zweiaxiger Kry-
stalle, 199.—K. Haushofer. Ueber das Verhalten des Dolomit gegen
Fissigsaure, 220.
Nancy. Société des Sciences. Bulletin. Série2. Tome iv. Fasc. 10
Gis79). 18380.
Fliche. Sur les lignites quaternaires de Jarville, 8.—Braconnier.
Description des terrains qui constituent le sol du département de Meurthe-
et-Moselle, 12.
_—_-,.
Tome iv. Fasc 11 (1880). 1880.
Nature. Vol. xxii. Nos. 556-574. 1880.
J.S. Gardner. A Chapter in the History of the Conifere, 199,—J.
268 ADDITIONS TO THE LIBRARY.
Milne. Seismology in Japan, 208.—T. S. Humpidge. New Metals,
232.—The Caribbean Sea, 242.—N.S. Maskelyne. Prof. W. H. Muller,
247.—Artificial Diamonds, 255.—A. Geikie. North-American Geology :
Idaho and Wyoming, 268.—J. S. Gardner. Observations on Arctic
fossil Floras with regard to Temperature, 341.—J. Murray. The Struc-
ture and Origin of Coral Reefs and Islands, 8351.—A. C. Ramsay. Address
to the British Association: On the Recurrence of certain Phenomena in
Geological Time, 383.—H. C. Sorby. Opening Address to the Geological
Section of the British Association, 390.—A. Geikie. A Fragment of
Primeval Europe, 400.—A. Agassiz. Paleeontological and Embryological
Development, 424.—British Association: Reports of Committees, 442 ;
Section C, Geology, 449.—H. B. Guppy. The Yang-tse, the Yellow
River, and the Pei-ho, 487.—Landslips, 505.—Richard Owen, 577.—A.
Zittel. The Geology of the Libyan Desert, 587.
Nature. Vol. xxiii. Nos. 575-600. 1880-81.
A. Geikie. The Lava-fields of North-western Europe, 3.—A. Murray.
Mineral Resources of Newfoundland, 46.—Curious Impressions in Cam-
brian Sandstone near Loch Maree, 93.—J. Thomson. Notes on the
Geology of East Central Africa, 102.—C. J. Merriman. Subterranean
Forest in India, 105.—British Earthquakes, 117.—A. Geikie. The
Mineralogical Society of Great Britain and Ireland, 150.—A. Geikie.
Geology of Bosnia and Herzegovina, 224.—J.S. Gardner. A Chapter
in the History of the Conifer, 251, 412.—_J. 8. Gardner. Geologising
at Sheppey, 293.—C. E. De Rance. The Blackheath Holes, 865.—Inter-
esting new Crinoids, 377.—Dr. J. J. Bigsby, 389.—The recent Discovery
of the Body of Rhinoceros Merckti in Siberia, 466.—Gold in Newfound-
land, 472.—V. Ball. On the Identity of some ancient Diamond-mines
in India, especially those mentioned by Tavernier, 490.—H. J. Johnston-
Lavis. The Earthquake in Ischia, 497.—C. E. De Rance. The Inter-
national Geological Congress, 510.—Achille Delesse, 535.—The new
Museum of Natural History, 549.—Dunes amd Moving Sand, 569.—Sir
Philip de Malpas Grey Egerton, 579.—C. A. Stevenson. Harthquake of
November 28, 1880, in Scotland and Ireland, 591.
. Vol. xxiv. Nos. 601-607. 1881.
T. G. Bonney. A Geologist’s Notes on the Royal Academy, 86.
Neuchatel. Société des Sciences Naturelles. Bulletin. Tome xii.
Cahier 1. 1880.
E. Desor. Sur la mer saharienne, 16.—Ritter. De l’action des vagues
sur les sables des bords du lac de Neuchatel, 114.
Newcastle-upon-Tyne. Natural-History Society &c. Natural-
History Transactions. Vol. vii. Part 2. 1880.
R. E. Hooppel. Presidential Address to the Members of the Tyneside
Naturalists’ Field Club, 187—W. Howchin. Notes on a Find of Pre-
historic Implements in Allendale, with Notices of similar Finds in the
surrounding District, 210.—J. Wright. Short Memoir of the Life of
Thomas Belt, F.G.8., 235.—Hugh Miller. Tyneside Hscarpments: their
Preglacial, Glacial, and Postglacial Features, 285.—R. Howse. Pre-
liminary Note on the Discovery of old Sea-caves and a raised Sea-beach
at, Whitburn Lizards, 8361.—R. Howse. Note on the Priority of Discovery
of Anodon Jukesti, Forbes, in the Lower Carboniferous Rocks of North
Northumberland, 376.
—. North-of-England Institute of Mining Engineers. Trans-
actions. Vol. xxix. (1879-80). 1880.
ADDITIONS TO THE LIBRARY, 269
New Haven, Conn. American Journal of Science. Ser. 3. Vol. xx.
Nos. 115-120. 1880.
J.D. Dana. Geological Relations of the Limestone Belts of West-
chester County, N. Y., 21, 194, 359, 450.—C. A. White. Antiquity of
certain subordinate Types of Fresh-water and Land Mollusca, 44.—
C. U. Shepard. Mineralogical Notices, 54.—J. M. Stillman. Bernar-
dinite; its Nature and Origin, 93.—G. J. Brush and E. 8. Dana. On
Crystallized Danburite from Russell, St. Lawrence, New York, 111.—
J. F. Whiteaves. On a new Species of Prerichthys, allied to Bothrio-
lepis ornata, Eichwald, from the Devonian Rocks of the North Side
of Baie des Chaleurs, 132.—C. D. Wallcott. The Permian and other
Paleozoic Groups of the Kanab Valley, Arizona, 221.—O. C. Marsh.
Notice of Jurassic Mammals representing two new Orders, 235.—G. J.
Brush and E. 8. Dana. Mineral Locality at Branchville, Connecticut :
(fourth paper) Spodumene and the Results of its Alteration, 257.—A.
Agassiz. Paleontological and Embryological Development, 294, 375.—
J. W. Dawson. Revision of the Land Snails of the Paleozoic Era, with
Descriptions of new Species, 403—W. O. Crosby and G. H. Barton.
Extension of the Carboniferous Formation in Massachusetts, 416.—E. T.
‘Cox. Discovery of Oxide of Antimony in extensive Lodes in Sonora,
Mexico, 421.—H. 8. Willams. Abstract of some Paleontological Studies
of the Life History of Sprrifer levis, H., 456.
ooo
: : . Vol. xxi. Nos. 121-126. 1881.
G. W. Hawes. The Albany Granite, New Hampshire, and its Contact
Phenomena, 21.—C. Barrois. Review of Professor Hall’s recently pub-
lished Volume on the Devonian Fossils of New York, 44.—Earthquake
at the Philippine Islands, of July 1880, 52.—W. H. Dall. Notes on
Alaska and the Vicinity of Behring Strait, 104.—S. H. Seudder. Relation
of Devonian Insects to later and existing Types, 111.—C. U. Shepard.
Meteoric Iron of Lexington Co., 5. C., 117.—G. F. Wright. Date of the
Glacial Era in Eastern North America, 120.—P. Collier. A remarkable
Nugget of Platinum, 123.—R. P. Whitfield. A new Genus and Species
of Air-breathing Mollusk from the Coal-measures of Ohio, 125.—J. L.
Smith. Hiddenite,a Variety of Spodumene, 128.—S. W. Ford. Remarks
on the Genus Obolella, 13i.—H. M. Chance. The Millstone Grit in
England and Pennsylvania, 134.—O. C. Marsh. Principal Characters
of American Jurassic Dinosaurs, 167.—S. H. Scudder. Structure and
Affinities of Zuphoberia of Meek and Worthen, 182.—C. G. Rockwood.
Recent American Earthquakes, 198.—G. W. Hawes. Liquid Carbon
Dioxide in Smoky Quartz, 203.—A. W. Wright. Gaseous Substances
contained in Smoky Quartz of Branchville, Conn., 209.—W. C. Kerr.
Origin of new Points in the Topography of North Carolina, 216.—W. P.
Blake. Occurrence of Realgar and Orpiment in Utah Territory, 219.—
O. C. Marsh’s Monograph on tht Odontornithes or Toothed Birds of
North America, 255.—W. E. Hidden. Whitfield County, Georgia,
Meteoric Iron, 286.—J. EK. Hilgard. The Basin of the Gulf of Mexico,
988.—E. A. Smith. The Geology of Florida, 292.—G. J. Brush. On
American Sulpho-Selenides of Mercury, with Analyses of Onofrite from
Utah by W. J. Comstock, 312.—H. 8. Williams. Channel-fillings in
Upper Devonian Shales, 318.—O. C. Marsh. New Order of extinct
Jurassic Reptiles (Cceluria), 539.—O. C. Marsh. Discovery of a fossil
Bird in the Jurassic of Wyoming, 341.—O. C. Marsh. American Ptero-
dactyles, 342.—W. C. Kerr. Action of Frost in the Arrangement of
superficial Earthy Material, 345.—N. H. Winchell. Dall’s Observations
on Arctic Ice, and the Bearmeg of the Facts on Glacial Phenomena in
Minnesota, 358.—J. P. Cooke. William Hallowes Miller, 379.—G. M.
270 ; ADDITIONS TO THE LIBRARY.
Dawson. Geology of Peace-River Region, 891.—O. C. Marsh. American
Jurassic Dinosaurs, 417.—J. D. Dana. Geological Relations of the
Limestone Belts of Westchester County, New York: South Westchester
County and Northern-New- York Island, 425.—J. L. Smith. Nodule of
Chromite in the Interior of compact Meteoric Iron from Cohahuila, 461.
J. F. Whiteaves. Fossil Fishes from the Devonian Rocks of Scaumenac
Bay, in the Province of Quebec, 494.—O. C. Marsh. New Jurassic
Mammals, 511.
New Haven, Conn. Peabody Museum of Yale College. Memoirs.
Moluis) S30:
O. C. Marsh. Odontornithes: a Monograph on the extinct Toothed
Birds of North America, 1.
New York. Lyceum of Natural History. Annals. Vol. xi. No.
13 (Index and Contents). 1876.
: . N.S. Volii.) Nos. 9-135) te7gSsu:
A. A. Julien, On Spodumene and its Alterations, 318.
—
r)
New York. The Engineering and Mining Journal. Vol. xxxi.
Nos. 1-11, 18-22. 1881. Presented by Dr. C. Le Neve
Foster, F.GS.
AC? Campbell. The Copper and Iron-bearing Rocks of Lake Su-
perior, 20.—W. B. Devereux. Gold and its aeeO aves Minerals at
King’s } Mountain, North Carolina, 59. The Mica Veins of
North Carolina, 211.—A. Murray. The Gold Ree near Brigus, New-
foundland, 252. “The Gold Mines of the Rhetian ‘Alps, 281.—J. 8. New-
berry. The Genesis of our Iron Ores, 286, 298.—I’. M. F. Cazin. The
Triassic Age of Sand-Rock carrying ores oe Copper and Silver, and the
origin of these Ores, 300.—The History of Tin, 313.—The Geological
formation, Tombstone, Arizona, 316.
Norwich Geological Society. Proceedings. Vol.i. Part 5. 1881.
H. B. Woodward. Ona Disturbance of the Chalk at Trowse, 109.—
J. Reeve. Additions to List of Fossils from the Norwich Crag at
Bramerton, 110.—H. Norton. On the Paleontology of the Ancients
(Greeks and Romans), 110.—A. J. Jukes Browne. ‘The Subdivisions of
the Chalk, 113.—J. H. Blake. Well-boring at Hast Dereham Water-
works, 126, —C. Reid. Well-boring at Cromer Waterworks, 129.—H.
Norton. Derivation of the Word “ Paramoudra,” 132.—J. H. Blake. On
the Age and Relation of the so-called Forest-bed of the Norfolk and
Suffoll: Coast, 137.
Norwich. Science Gossip Club. ‘Report of Proceedings at the
Annual Meeting, June 11, 1874. 1874. Presented by H. B.
Woodward, Esq., F.GS. :
. Report of Proceedings at the Annual Meetings
June 6, 1877, and May 14, 1878. 1878(?). Presented by
Ed Woodward, Esq., PGS.
S. ©. Sothern, Presidential Address, 6.—H. B. Woodward. Presi-
dential Address, 29. |
Nottingham. The Forester, or the Nottingham-High-School Maga-
zine. Vol. i. 1878. Presented by W. Whitaker, Esq., £.GS.
ADDITIONS TO THE LIBRARY. 271
Nottingham. The Forester, or the Nottingham-High-School Maga-
ame,” Vol. it. 1879. ‘Presented “by W. Whitaker, Esq.,
GS.
The Sandstones of the Carboniferous and Triassic Rocks, 68.—Geo-
logical Excursion to Charnwood Forest, 94.
. —. Vol. ni. 1880. Presented by W. Whitaker, Ksq.,
F.GS.
The Origin of Sandstones, 36.
Paleontographical Society. Monographs. Vol. xxxv. (1881). 1881.
(Two copies.)
T. Wright. The Cretaceous Echinodermata, vol. i. part 9.—T. David-
son. Supplement to the Fossil Brachiopoda, vol. iv. part 4.—J. Lycett.
The Fossil Trigoniz : Supplement.—T. Wright. The Lias Ammonites,
Part 4—R. Owen. The Reptilia of the Liassic Formation, Part 3.—
L. Adams. The Fossil Elephants (£. primigenius and meridionalis),
Part 3.
Paris. Académie des Sciences. Comptes Rendus. Tome xcii.
Nos. 1-24.. 1881.
W. L. Green. Nouvelle irruption du Mauna-Loa (iles Hawai), 48.—
A. Daubrée. Substances cristallines produites aux dépens de médailles
antiques, immergées dans les eaux thermales de Haracci, commune
d’Olmeto (Corse), 27.—A. Daubrée. Production contemporaine du soufre
natif dans le sous-sol de Paris, 101.—B. Studer. Le contact mécanique
du gneiss et du calcaire, dans i’Oberland bernois, observé par M. A.
Baltzer, 169.—A. Daubrée. Hxamen de matériaux provenant de quelques
forts vitrifiés de Ja France; conclusions qui en résultent, 269.—D. Col-
ladon. Sur le tremblement de terre qui a été ressenti en Suisse, le 27
janvier 1881, 530.—S. Meunier. Examen lithologique et géologique de
la météorite tombée le 13 Octobre 1872 aux environs de Soko-Banja, en
Serbie, 331.—F. Fouqué et A. M. Lévy. Reproduction artificielle des
basaltes, 367.—A. Daubrée. Sur les réseaux de cassures ou diaclases qui
coupent la série des terrains stratifiés; nouveaux exemples fournis par
les couches crétacées aux environs d’Htretat et de Dieppe, 393.—A. Cara-
ven-Cachin. Ancienneté de lElephas primigenius (Blum.) dans le bassin
sous-pyrénéen, 475.—Desor. Ossements humains trouyvés dans le dilu-
vium de Nice; examen de la question géologique, 746.—Niepce. Osse-
ments humains trouvés dans le diluvium de Nice; description des
ossements, 749.—Quatrefages. Ossements humains trouvés dans le
diluvium de Nice; détermination de la race, 750.—A. Gaudry. Sur un
nouveau genre de poisson primaire, 752.—A. Julien. Sur l’existence et
les caractéres du terrain cambrien dans le Puy-de-Déme et dans |’ Aller,
754.—Dieulafait. Loi générale de formation des eaux minérales salines ;
application au cas particulier de Gréoux (Basses-Alpes), 756.—L. Crié.
Sur la découverte, a Noirmoutiers (Vendée) de la flore éocéne a Sabalites
andegavensis, Sch.,759.—A. Julien. Sur la nature et Vordre d’apparition
des roches éruptives anciennes que l’on observe dans la région des volcans
a cratéres du Puy-de-Dome, 799.—Des Cloizeaux et Damour. Note sur
la chaleoménite, nouvelle espéce minérale (sélénite de cuivre), 837.—
J. L. Smith. Anomalie magnétique du fer météorique de Sainte-Cathe-
rine, 843.—Mayencgon. Sur la bismuthine produite par les houilléres
incendiées, 854.—F’. Fouqué et A. Michel Lévy. Reproduction arti-
ficielle des diabases, dolérites et météorites 4 structure ophitique, 890.—
A. Julien. Sur le terrain dévonien de Diou (Allier) et de Gilly (Sadéne-
et-Loire), 891.—H. Filhol. Sur les différentes espéces d’Ours dont les
272 ADDITIONS TO THE LIBRARY.
débris sont ensevelis dans la caverne de Lherm (Ariége), 929.—Le Cha-
telier. Production d’un silicate de baryte hydraté en cristaux, 931.—
EK. Mallard. Sur la production d’un phosphure de fer cristallisé et du
feldspath anorthite, dans les incendies des houilléres de Commentry, 933.
De Pellissier. Sur le tremblement de terre de Chio, 956.—G. Rolland.
Sur les grandes dunes de sable du Sahara, 968.—A. Daubrée. Examen
de matériaux provenant des forts vitrifiés de Craig Phadrick, prés Inver-
ness (Ecosse) et de Hartmannswillerkopf (Haute-Alsace), 980.—A.
Daubrée. Météorite tombée & Louans (Indre-et-Loire) le 25 janvier
1845 et dont la chute est restée inédite, 984.—Lawrence Smith. Nodule
de chromite dans Vintérieur du fer météorique de Cohahuila (Mexique)
(météorite de Butcher), 991.—F. Fouqué. Sur la série stratigraphique
des roches qui constituent le sol de la haute Auvergne, 1089.—F. Fouqué
et M. Lévy. Hxamen de quelques produits artificiels de James Hall,
1040.—E. Filhol. Sur quelques feldspaths de la vallée de Bagnéres-de-
Luchon (Haute-Garonne), 1059.—A.Gaudry. Sur les plus anciens rep-
tiles trouvés en France, 1145.—H. Fayol. Etudes sur le terrain houiller
de Commentry, 1172.—G. de Saporta et A. F. Marion. Sur les genres
Williamsonia, Carruth. et Goniohna, VOrb., 1185, 1268.—F. Pisani. Sur
un vanadate de plomb et de cuivre du Laurium, 1292.—A. Julien. Sur
Vexistence du terrain cambrien a Saint-Léon et Chatelperron (Allier),
1293.—H. Fayol. Sur le terrain houiller de Commentry; expériences
faites pour en expliquer la formation, 1296.—De Lesseps. Sur le rap-
port de M. le commandant Roudaire, relatif 4 sa derniére expédition dans
les chotts tunisiens, 1309.—K. Hébert. Observations sur les résultats
géologiques fournis par les missions de M. le commandant Roudaire dans
les chotts tunisiens, 1510.—A. Damour. Nouvelles analyses sur la jadeite
et sur quelques roches sodiféres, 1312.—C. Friedel et E. Sarrasin. Sur
la reproduction par voie aqueuse du feldspath orthose, 1874.—A. Julien.
Sur la faune carbonifére de Régny (Loire) et ses relations avec celle de
V’Ardoisiére (Allier), 1451.
Paris. Annales des Mines. Série 7. Tome xvii. 2° et 3° livr. de
1880. 1880.
Delesse et de Lapparent. LExtraits de géologie pour les années 1877
et 1878, 209.—Petiton. Note sur les mines de l’archipel des Ferde (iles
de Sudérée et de Naalsde), 305.—F. Rigaud. Notice sur les travaux
exécutés 4 Bourbonne-les-Bains, 349,
Tome xviii. 4°-6° livr. de 1880. 1880.
E. Boutan. Note sur la constitution géologique de Visthme de Panama,
au point de vue de l’exécution du canal interocéanique, 5.—H. Sauvage.
Notice sur les sources minérales des départements de Seine-et-Oise, de
Seine-et-Marne et du Loiret, 102.—Ferrand. Notice sur les mines
d’anthracite de la Mure, 121.—A. Carnot. Note sur deux variétés de
diadochite (phosphosulfate de fer) trouvées dans la mine d’anthracite de
Peychagnard (lsére), 148.—G. Rolland. Mission transsaharienne de
Laghouat, El-Goléah, Ouargia, Biskra: géologie et hydrologie, 152.—
Domeyko. Note sur des cristaux épigénes de cuivre métallique prove-
nant des mines de cuivre de Coro-Coro en Bolivie, 531.—Domeyko.
Note sur les minéraux de bismuth de Bolivie, du Pérou et du Chili,
538.
: 4 Tome xix. 1%e livr.de 1881. 1881.
Villot. Note sur le régime de la source de Camoins-les-Bains (com-
mune de Marseille), 5, 157.—M. Du Chatenet. Htat actuel de Vindus-
trie minérale dans le Cerro de Pasco, 61.
ADDITIONS TO THE LIBRARY. 273
Paris. Annales des Sciences Géologiques. Tomex. 1879. Pur-
chased.
C. Barrois. Mémoire sur le terrain crétacé du bassin d’Oviédo, No. 1.—
Cotteau. Notice sur les Echinides urgoniens recueillis par M. Barrois
dans la province d’Oviédo (Hspagne), No. 2.—H. Filhol. Etude des
mammiféres fossiles de Saint-Géraud le Puy (Allier), No. 3.
: Tome xi. Nos.1&2. 1880. Purchased.
H. Filhol. Etude des mammiféres fossiles de Saint-Géraud le Puy
(Allier), 1, 49.
Pe Hobart.
——. Annales des Sciences Naturelles. Série 6. Zoologie et Pa-
léontologie. Tomeix. Nos. 1-6. 1880. Purchased.
«6 Lome x. Nos. 1-6. 1880. Purchased.
——. Annales Hydrographiques. Série 2. Tomei. 2° semestre
1879. 1879. Presented by the Dépét de la Marine.
a ~=—index to vols. xxix. to xit. 1879,
Nome) xa. Nos) Po& 2.) 1830.- Presented by
——. Association francaise pour lVAvancement des Sciences.
Compte-rendu de la 8° Session (Montpellier, 1879). 1880.
Purchased.
Garrigou. Des sources minérales mercurielles de la France, analyse
des eaux minérales, 474.—A. Toucas. Notice sur le terrain crétacé des
Corbiéres, 574.—V. Lemoine. Sur les ossements fossiles des terrains
tertiaires inférieurs des environs de Reims, 585.—E. Riviére. De quelques
hyperostoses de poissons trouvées dans les grottes quaternaires de Menton
en Italie, 595.—F. Pommerol. Le mouflon quaternaire, 600.—A. Jean-
jean. tude sur l’oxfordien supérieur, le corallien et le néocomien infé-
rieur, dans les Cévennes, 610.—P. de Loriol. Les crinoides fossiles de
la Suisse, 627.—C. Grad. Sur la formation des charbons feuilletés gla-
ciaires de la Suisse, 636.—Cazalés de Fondouce. Erosion de cailloux
quaternaires due 4 l’action du vent et du sable, 646.—P. de Loriol. Note
sur les échinides recueillis dans les expéditions du ‘Challenger’ et du
‘Blake, 650.—G. Cotteau. Considérations stratigraphiques et paléon-
tologiques sur les échinides de l’étage cénomanien de l’Algérie, 655,—
Moriére. Note sur une station de silurien 4 la Bréche-au-diable (Cal-
vados), 663.—C. Barrois. Sur l’étendue du systéme tertiaire inférieur
dans les Ardennes et sur les argiles a silex, 666.—C. Barrois. Sur le
marbre griotte des Pyrénées, 668.—C. Barrois. Sur la faune troisiéme
silurienne du Finistére, 669.—E. Riviére. Le pliocéne de Castel d’Appio
en Italie, nomenclature des fossiles quwil renferme, 670.—Ollier de
Marichard. Les troglodytes de ’Ardéche ou premiére page inédite de
Vhistoire du Vivarais, 797.—Pommerol. Le gisement quaternaire de
Sarliéve, 301—F. Daleau. Les stations préhistoriques des étangs
d@Hourtin et de Lacanau (Gironde), 807.—P. Fiére. Grottes préhis-
toriques du Dauphiné, 852.
Paris. Dépot de la Marine. Annuaire des Marées des cétes de
France pour ’an 1881. 1880.
——. Journal de Conchyliologie. Série 3. Tome xx. Nos. 3 et 4.
1880. Purchased.
R. Tournouér. Description d’un Ostrea fossile de la mollasse miocéne
VOL, XXXVII. x
274 ADDITIONS TO THE LIBRARY,
de Forcalquier, Basses-Alpes, 256.—H. Douvillé. Sur la forme de
Vouverture de ? Ammonites pseudo-anceps, 355.
Paris. Journal de Conchyliologie. Serie 3. Tome xxi. No. 1.
Purchased.
——. Muséum d’Histoire Naturelle. Nouvelles Archives. Série 2.
Tomenium.)/Hascylet 24) isso:
S. Meunier et J. Lambert. Recherches stratigraphiques et paléon-
tologiques sur les sables marins de Pierrefitte prés Htampes, Seine-et-Oise,
235.—A.T.de Rochebrune. Révision des ophidiens fossiles du Muséum
de histoire naturelle, 272.
Revue Scientifique de la France et de l’Etranger. Série 2.
Tome xix. Nos. 1-26. 1880.
Fouqué. De la pétrologie, de la place qu’elle doit occuper dans les
programmes universitaires et des modifications principales a apporter
dans ces programmes en ce qui regarde les sciences géologiques, 18.—
G. Rolland. La mission transsaharienne El Goleah, 53.—C. Velain.
La chorologie des sédiments et sa signification pour Ta géologie et la
théorie de la descendance, 204. —Friedel. La reprog ern des minéraux,
242.—C. Barrois. Paléontologi ie de |’ Etat de New York, 257.—J. Thoulet.
Contribution a V’étude des propriétés physiques et chimiques des miné-
raux microscopiques, 283.—J. Roche. La mission d’exploration trans-
saharienne, 505.—J. Bayol. La mission du haut Niger, 601.
. Tome xix. Nos. 1-25. 188ie
Faye. Des voleans de la lune, 130.—Les sources de naphte dans la
région du Caucase, 337.—C. Velain. L’Algérie et le pays des Kroumits,,
545.—G. Rolland. - Les orandes dunes de sable du Sahara, 609.
——. Société Géologique de France. Bulletin. Série 3. Tome vi.
(US 73)S Nosy Iréc LO rSss0:
A. Cordella. Note sur les mines du Laurium et sur les nouveaux gites
de mineral de zine (Smithsonite), 577.—Loustau et Belhomme. Note
sur un sondage exécuté a Monsoult (Seine-et-Oise), 581.—G. Dollfus.
Observations sur le sondage de Monsoult, 585.—Bonneau du Martray.
Note sur un bloc erratique situé dans la yallée de la Dragne, prés de
Moulins-Engilbert (Niévre), a 2 kilométres environ de la faille occiden-
tale du Morv van, 098.—Torcapel. Les glaciers quaternaires des Cévennes,
600.—Daubrée. Expériences sur la production de déformations et de
cassures par glissement, 608.—Potier. Sur la direction des cassures dans
les corps isotropes, 609.—H¢hert et Munier-Chalmas. Recherches sur
les terrains tertiaires du Vicentin, 610, 619.—R. Zeiller. Sur une nou-
velle espéce de Decranophyllum, 611 —Leymerie. Observations sur le
mémoire de M. Peron sur les calcaires a Echinides des bains de Rennes,
616.—Peron. Réponse aux observations de M. Leymerie, 616.—Cotteau.
Sur Vexposition géologique et paléontologique du Havre, 618.—Tournouer.
Sur les cérites des marnes a Happarion du puits Kharoubi, prés Oran,
618.—Tournouer. Sur les coquilles marines trouvées dans la région des
chotts sahariens, 619.—K. Riviére. Note sur la grotte de Grimaldi, 621.
—Sauvage. Note sur les poissons fossiles, 625.—Tardy. De la limite
entre le Crétacé et le Tertiaire aux environs de Vitrolles (Bouches-du-
Rhone), 637.—C. Vélain. Compte- -rendu de l’excursion 4 Meudon, 654.
—Tournouér. Compte-rendu de l’excursion 4 Etampes, 663. —De Lap-
parent. Hxcursion dans le pays de Bray, 675.—De Mercey.. Compte-
rendu de Vexcursion a Maigneley, 679.—O. Vélain. Compte-rendu de
Vexcursion de la Frette a Sannois, 687.—H. Douvillé. Compte-rendu de
Vexcursion & Vernon (1° partie), 694.—De Chancourtois. Compte-rendu
ADDITIONS TO THE LIBRARY. 275
de Vexcursion a Vernon (2° partie), 697.—De Chancourtois. Sur les
alionements géologiques relevés dans les environs de Vernon, 703.—H.
Douyillé. Résumé de l'état de la question des sables dits éruptifs, 706.
—C. Vélain. Compte-rendu de l’excursion a Cuise-la-Motte, 711.
Paris. Socicté Géologiquede France. Bulletin. Série 3. Tome vii.
(1879). Nos. 5-8. 1880.
C. Vélain. Sur la constitution géologique des iles Seychelles, 278.—
A. Falsan. Sur la position stratigraphique des terrains tertiaires supéri-
eurs et quaternaires & Hauterives (Dréme), 285.—A. Locard. Observa-
tions paléontologiques sur les couches a Ostrea Falsani dans les environs
de Hauterives (Drome), 307.—A. de Lapparent. Note sur l’ouvrage de
M. Struckmann intitulé “ Le Jura supérieur des environs de Hanovre,”
315.—G. Dollfus. Les dépdots quaternaires du bassin de la Seine, 318.—
A. de Lapparent. Sur la disposition générale des reliefs du globe ter-
restre, 346.—N. de Mercey. Remarques sur la classification du terrain
crétacé supérieur, 355.—Tournouér. Sur l'étude du bassin de Visan par
M. Fontannes, 587.—C. Vélain. Notes géologiques sur la Haute-Guy-
ane, d’aprés les explorations du Dr. Crevaux, 388.—V. Lemoine. Oi-
seaux fossiles des terrains tertiaires inférieurs des environs de Reims,
398.—F. Delafond. Note sur l’existence du terrain néocomien aux envi-
rons de Tournus (Saéne-et-Loire), 403.—E. Hébert. Sur la position des
sables de Sinceny, 408.—A. Boué. Sur la vallée de la Soukava, 412.—
C. Vélain. Ile de Pagues, 415.—Delage. Etude du calcaire de Lorman-
diére, 426.—Meugy. Observations sur une note de M. Barrois, relative au
terrain crétacé des Ardennes, 445.—Lebesconte. Sur le bassin tertiaire
des environs de Rennes, 451.—Tournouér. Etude sur les fossiles de
létage tongrien (d’Orbigny) des environs de Rennes en Bretagne, 464.—
E. Benoit. De Vextension géographique et stratigraphique du purbeckien
dans le Jura, 484.—F. Fontannes. Note sur la découverte de deux
espéces nouvelles du genre Antedon dans les terrains tertiaires supérieurs
du bassin du Rhéne, 497.—Tardy. Le dernier diluvium quaternaire,
500.—Tardy. Deuxiéme note sur le chronométre de la Sadne, 514.—
A. Gaudry. Allocution présidentiel, 517.—KH. Jannettaz. Notice nécro-
logique sur M. G. Delafosse, 524.—L. Lartet. Vie et travaux d’Alex-
andre Leymerie, 530.—V. Lemoine. Note sur les ossements fossiles des
terrains tertiaires inférieurs des environs de Reims, 558.—Rey-Lescure.
Carte géologique de Tarn-et-Garonne, 562.
: : i Tome vii. Séance Generale An-
nuelle et Célébration du Cinquantenaire de la Société. 1880.
Penzance. Royal Geological Society of Cornwall. Transactions.
Wolke: Part 3. 1331.
A. P. Vivian. Presidential Address, Ixxxvi.—W. A. E. Ussher.
Pleistocene Notes on the Cornish Coast between Plymouth and Looe, 68.
—W. A. E. Ussher. The Devonian Rocks between Plymouth and East
Looe, 70.—W. W.Smyth. On the Occurrence of Feather Ore (Plumosite)
in Foxdale Mine, Isle of Man, 82.—C. W. Peach. On Fossils’ from the
Rocks of Cornwall, some of them new to the list, 90.—J. H. Collins. Note ©
on the Occurrence of Stanniferous Deer-horns in the Tin-gravels of Corn-
wall, 98.—J. H. Collins. Note on the supposed Serpentine of the Parish
of St. Veep, 101.—R. N. Worth. Notes on the Geology of the South-east
Border of Cornwall, 103.
Philadelphia. Academy of Natural Sciences. Journal. Series 2.
Vol. viii: Part 4. 1881.
W.M. Gabb. Description of Caribbean Miocene Fossils, 8337.—W. M.
Gabb. Description of new Species of Fossils from the Pliocene Clay Beds
“2
276 ADDITIONS TO THE LIBRARY.
between Limon and Moen, Costa Rica, together with Notes on previously
known Species from there and elsewhere in the Caribbean Area, 349.
Philadelphia. Academy of Natural Sciences. Proceedings, 1880.
Parts 1-3. 1880.
A. Heilprin. On the Stratigraphical Evidence afforded by the Tertiary
Fossils of the Peninsula of Maryland, 20.—A. W. Vogdes. Description
of a New Crustacean from the Upper Silurian of Georgia, with Remarks
upon Calymene Clintoni, 176.—T. D. Rand. Serpentine Belts of Radnor
Township, Delaware Co., 225.—H. C. Lewis. A Garnet with inverted
Crystallization, 241.—T. D. Rand. Change of Serpentine into Quartz,
241.—H. C. Lewis. Magnetite Markings in Muscovite, 242.—H. C.
Lewis. The Optical Characters of some Micas, 244.—H. C. Lewis. On
an exfoliated Talc, 252.—H. C. Lewis. Tin in North Carolina, 253.—
H. C. Lewis. On Siderophyllite, a new Mineral, 254.—H. C. Lewis.
On Sterlingite and Damourite, 256.—H. C. Lewis. Vanadium in Phila-
delphia Rocks, 256.—H. C. Lewis. The Surface Geology of Philadelphia
and Vicinity, 258.—T. D. Rand. On Randite, 274.—T. D. Rand. Some
microscopic Enclosures in Mica, 276.—H. C. Lewis. On the Bryn-Mawr
Gravel, 277.—H. C. Lewis. On some Enclosures in Mica, 278.—H. C.
Lewis. On Dendrites, 278.—H. C. Lewis. On a Jurassic Sand, 279.—
H. C. Lewis. The Minerals of Surry Co., N. C., 280.—T. D. Rand. On
a, peculiar Stratification in Gneiss, 280.—H. C. Lewis. A new Locality
for Lignite, 281.—H. C. Lewis. On Serpentine in Bucks Co., 281.—
H. C. Lewis. The Iron Ores and Lignite of the Montgomery-Co. Valley,
282.—H. C. Lewis. An Enclosure in Quartz, 292.—W. W. Jefferis.
Menaccanite and Tale from Maryland, 292.—W. W. Jefferis. Sandstone
in Labradorite, 292.—A. E. Foote. On a probable Pseudomorphism of
Gumuite and Uranotite after Uraninite, 292.—H. C. Lewis. Ona new Fu-
coidal Plant from the Trias, 293.—T. D. Rand. The northern Belt of Ser-
pentine in Radnor Township, 295.—H.C. Lewis. The Trenton Gravel and
its Relation to the Antiquity of Man, 296.—H. C. Lewis. Note on Phila-
delphite, a new Mineral, 310.—R. Haines. Analysis of Philadelphite,
310.—F. A. Genth, jun. The so-called Emery-ore from Chelsea, Bethel
Township, Delaware Co., 311.—H. C. Lewis.—On Philadelphite, 313.—
H. C. Lewis. A Potsdam-Sandstone Outcrop on the 8. Valley Hill of
Chester Valley, 329.—G. A. Konig. Notes on Jarosite, 331.—J. Leidy.
Bone Caves of Pennsylvania, 546.—A. Heilprin. On some new Lower-
Eocene Mollusca from Clarke Co., Alabama, with some Points as to the
stratigraphical Position of the Beds containing them, 364.
Philadelphia. American Philosophical Society. Proceedings. Vol.
xvii. Nos.105 & 106. 1880.
C. A. Ashburner. On the Oil-sand of Bradford, M‘Kean County, 419.
—C. E. Hall. Relations of the Crystalline Rocks of Pennsylvania to the
Silurian Limestones, and the Hudson-River Age of the Hydromica Schists,
435.
Photographie Society of Great Britain. Journal and Transactions.
NESS Wolves wNoycamlcod:
: Vol. v. Nos. 1-7. 1880-81.
Physical Society. Proceedings. Vol. ii. Part 4. 1880.
WVoliive catty en loole
Pisa. Societa toscana di Scienze Naturali. Atti. Processi verbali.
Vol. ii. pp. 89-232. 1880-81.
S. de Bosniaski. La formazione gessoso-solfifera e il secondo piano
ADDITIONS TO THE LIBRARY. 27
mediterraneo in Italia, 90.—G. Meneghini. Nuovi fossili delle Alpi
apuane, 102.—M. Canavari. Di alcuni ammoniti del lias medio rac-
colti nelle vicinanze diS. Antonio nel gruppo montano di Tivoli, 109.—
D. Pantanelli. NRadiolarie nei calcari, 111.—A. Manzoni. Ciottoli im-
prontati, 112.—C. de Stefani. Carte geologiche delle Calabrie meridio-
nali, 113.—C. de Stefani. Il Tortoniano dell’ alta val di Tevere, 114.—
C. de Stefani. I fossili di Dicomano in Toscana e della Porretta nel
Bolognese, 115.—C.de Stefani. Natura dei battrilli, 116.—C. de Stefani.
Il gault e la creta superiore nell’ Apennino settentrionale, 117.—C. de
Stefani. Ordinamento cronologico dei terreni delle Alpi apuane, 118.—
F, Castelli. Delfino fossile, 131.—C. de Stefani. Il miocene di Canipa-
rola, 140.—C. de Stefani. Osservazioni ad alcune pubblicazioni geolo-
giche del R. Comitato geologico italiano sulle Alpi apuane, 141.—C.
de Stefani. Pieghe costituenti le Alpi apuane, 156.—A. D’Achiardi.
Su di alcuni minerali della miniera del Frigido presso Massa nelle Alpi
apuane, 171.—D. Zaccagna. In risposta alle osservazioni del De Stefani
sopra alcune pubblicazioni geologiche del R. Comitato geologico italiano
sulle Alpi apuane, 179.—B. Lotti. In risposta alle osservazioni del De
Stefani sopra alcune pubblicazioni geologiche del RK. Comitato geologico
italiano sulle Alpi apuane, 186.—G. Meneghini. Ammoniti del lias
medio, 188.—C. de Stefani. Di nuovo sui lavori del Comitato geologico
nelle Alpi apuane, 189.—M. Canavari. Alcuni nuovi Brachiopodi degli
strati a Terebratula aspasia Meh. nell’ Appennino centrale, 197.—D. Pan-
tanelli. Su alcune rocce della Montagnola senese, 197.—G. Meneghini.
Nuovi trilobiti di Sardegna, 199.—C. de Stefani. Studi microlitologici
pel paleozoico e pel trias delle Alpi apuane, 202.—C. de Stefani. Il
macigno di Porretta ed i terreni corrispondenti, 206.—C. de Stefani.
Origine degli strati pontici intorno al Mediterraneo, 209.—C. de Stefani.
Sui terreni marini dell’ epoca postpliocenica, 212.—C. de Stefani. Le
pieghe dell’ infralias nelle Alpi apuane, 216.—S. de Bosniaski. Una
pianta fossile del Verrucano dei monti pisani, 219.—S. de Bosniaski. Le
argille da stoviglie del Camerinese, 221.—S. de Bosniaski. L’eta geolo-
gica dei monti della Tolfa, 222.—Forsyth Major. Sgualodon quaternarium,
227.—Forsyth Major. Studii sugli avanzi pliocenici del genere Sus (Sus
Strozzt Menegh.), 227.
Pisa. Societa toscana di Scienze Naturali. Atti. Memorie. Vol. iv.
fase. 2. 18380.
M. Canavari. Sui fossili del lias inferiore nell’ Appennino centrale,
141.—G. Grattarola e F.Sansoni. Studii chimici sulla heulandite e sulla
stilbite di S. Pietro (Elba) etc., 173.—G. Grattarola. Beccarite, varieta
di zircon di Ceylon, 177.—R. Lawley. Nuovi denti fossili di Motedanus
rinvenuti ad Orciano pisano, 196.—G. Grattarola. Orizite e pseudona-
trolite, due nuove specie del sott’ordine delle zeoliti, 226.—A. D’Achiardi.
Coralli giurassici dell’ Italia settentrionale, 233.—F. Sansoni. Sulle
zeoliti dell’ isola d’Elba, 311.—A. Manzoni. Echinodermi fossili plioce-
nici, 8327.—G. Meneghini. TF ossili oolitici di Monte Pastello nella pro-
vincia di Verona, 336.
Plymouth. Devonshire Association for the Advancement of Science,
Literature, and Art. Report and Transactions. Vol. xii.
1880.
W. A. E. Ussher. Physical Features of Devonshire, 251.—A. R.
Hunt. Notes on the Submarine Geology of the English Channel off the
Coast of South Devon, 291.—W. Pengelly. Notes on Boulders and
Scratched Stones in South Devon, 304.—N. Worth. Recent Geological
Discoveries in the Neighbourhood of Plymouth, 361.—W. Downes
27 8 ADDITIONS TO THE LIBRARY.
Blackdown, 420.—W. Pengelly. Notes on recent Notices of the Geology
and Paleeontology of Devonshire, 591.
Plymouth Institution and Devon and Cornwall Natural-History
Society. Annual Report and Transactions. Vol. vii. Part 2.
1880. |
W. Sharman. Darwinism, 218.—F. J. Webb. Natural History of
Coal, 293.—F. Brent. The Stone Implements, 295.
Popular Science Review. New Series. Vol. iv. Nos. 15 & 16.
1880. Purchased.
P. H. Carpenter. Feather-Stars, recent and fossil, 193.—J. F. Blake.
The Portland Building Stone, 205.—M. F. de Castro. On the Influence
which a molecular Movement, due to Electricity, may have exerted in
certain Geological Phenomena, namely the Metamorphism of Rocks and
the Formation of Metalliferous Deposits, 230.—P..M. Duncan. On the
Opinions of Voltaire and Laplace regarding Geology, 310.—J. Milne. A
large Crater, 336.
; . Vol.v. Nos. 17 &18. 1881. Purchased.
J.S. Gardner. The Permanence of Continents, 117.
Quekett Microscopical Club. Journal. Nos. 44-46. 1880-81.
Ray Society. A Monograph of the Free and Semiparasitic Copepoda
of the British Islands. By G. 8. Brady. Vol. ii. 8vo.
1880. |
-——. Monograph of the British Aphides. Vol. iii. By G. B.
Buckton. 8vo. 1881.
Riode Janeiro. Museu Nacional. Archivos. Vol.ii. Trimestres
3 e4, 1878.
O. A. Derby. A geologia da regiao diamantifera da Provincia do
Parana no Brasil, 89.—O. A. Derby. <A bacia cretacea da bahia de Todos
os Santos, 185.—R. Rathbun. Observacdes sobre a geologia aspecto da
Ilha de Itaparica, na bahia de Todos os Santos, 159.
Rome. Reale Accademia dei Lincei. Atti. Serie 3. Transunti.
Wolves Haseaielss 0:
Capellini e Meneghini. Sopra la memoria del Dott. D. Pantanelli, in-
titolata: I diaspri della Toscana e i loro fossili, 198.—Capellini e Meneghini.,
Sulla memoria del Dott. M. Canavari, dal titolo: I Brachiopodi degli
strati a Terebratula Aspasia, Mgh. nell’ Appennino centrale, 199.—Tara-
melli e Meneghini. Sulla memoria del Dott. C. F. Parona, intitolata: Il
calcare di liasico di Gozzano, e i suoi fossili, 201.—Cornalia e Capellini.
Sulla nota del Dott. A. Incoronato avente per titolo: Sopra uno scheletro
umano dell’ epoca della pietra della provincia di Roma, 201.—Ponzi. Sui
lavori del Tevere e sulle variate condizioni del suolo romano, 203.—G.
Terrenzi. II lias superiore nel versante orientale della catena montuosa
Narnese, 209.—Struever. Sulla Perowskite di Val Malenco, 210.—A.
Piccini. Analisi di un’ augite del Lazio, 224.—F. Mauro. Ricerche
chimiche sulle lave di Montecompatzi, del Tusculo, di Villa Lancellotti e
di Monte Pila, 226.—Cossa. Sulla diffusione dei metalli della Cerite,
232.—Cossa. Sultungstato di didimio, 233.—Cossa, Sopra un granato
verde di Val Malenco, 254.
=. Vol. vi Fase) 122 iiseme
R. Meli. Sulla natura geologica dei terreni incontrati nelle fondazioni
tubulari del nuovo ponte in ferro costruito sul Tevere a Ripetta, e sull’
ADDITIONS TO THE LIBRARY. 279
Unio sinuatus, Lamk. rinvenutovi, 21.—Cornalia. Due piccoli imenotteri
fossili dell’ ambra siciliana, 80.—A. Cossa. Sulla stilbite del ghiacciaio
del Miage (Monte Bianco), 86.—A. Cossa. Sulla Ollenite, roccia anfibo-
lica del monte Ollen, 88.—Meneghini e Capellini. Sulla Memoria del
Prof. Seguenza “ Lo stretto de Messina,” 113.—Capellini. Resti di Tapiro
nella lignite di Sarzanello, 131.—Ponzi. Sui tufi vulcanici della Tuscia
romana, a fine di togliere qualunque discordanza di opinione emessa sulla
loro origine, diffusione, ed eta, 1382.—Pigorini, Cossa e Capellini. Sulla
memoria del Dott. D. Lovisato “Cenni critici sulla preistoria calabrese,”
195.
Royal Agricultural Society of England. Journal. Second Series.
Vol. xvi. Part 2. No. 32. 1880. 3
Vol. xvii. Part 1. 1881.
Royal Asiatic Society of Great Britain and Ireland. Journal. N.S.
Vol. xii, Parts3 & 4. 1880.
: Wolltoaire (Barts i 2) 1S3i:
Royal Astronomical Society. Memoirs. Vol. xlv. 1879-80. 1880.
Royal Geographical Society. Journal. Vol. xlix. (1879). 1880.
R. F. Burton. Itineraries of the Second Khedivial Expedition: Me-
moir explaining the new Map of Midian made by the Egyptian Staff-
officers, 1—R. F. Burton. A Visit to Lissa and Pelagosa, 151.—R. C.
Temple. An Account of the Country traversed by the Second Column
of the Tal-Cho’tia’li Field Force in the Spring of 1879, 190.—G. Rol-
leston. The Modifications of the external Aspects of Organic Nature
produced by Man’s Interference, 320.
——. Proceedings. Vol. ii. Nos. 7-12. 1883.
; . N.S. Vol. ii. Nos. 1-6. 1881.
W.-M. Crocker. Notes on Sarawak and Northern Borneo, 193.—J.
Stewart. Lake Nyassa and the Water Route to the Lake Region of
Africa, 257. |
Royal Institution of Great Britain. Proceedings. Vol. ix. Part 3.
No. 72. 1880.
W. B. Carpenter. Sea and Land in relation to Geological Time, 268.
Royal Microscopical Society. Journal. Vol. iii. Nos. 4—-6a. 1880.
H. Stolterfoth. On the Diatomaces in the Llyn Arenig Bach Deposit,
913.
Second Series. Vol: i. Parts1-3. 1881.
Ww. H. Shrubsole and F. Kitton. The Diatoms of the London Clay,
381.
Royal Society. Philosophical Transactions. Vol. clxxi. Parts 1-3.
1880-81.
W.C. Williamson. On the Organization of the fossil Plants of the
Coal-measures, Part X., including an Examination of the supposed Ra-
diolarians of the Carboniferous Rocks, 493.—G. H. Darwin. On the
Secular Changes in the Elements of the Orbit of a Satellite revolving
about a tidally-distorted Planet, 713.—R. Owen. Description of some
Remains of the gigantic Land-lizard (Megalania prisca, Owen) from
Australia, Part IT., 1037.
——, ——. Vol. clxxi. Part1. 1881.
280 ADDITIONS TO THE LIBRARY.
Royal Society. Proceedings. Vol. xxx. No. 205. 1880.
W.C. Williamson. On the Organisation of the fossil Plants of the
Coal-measures, Part XJ., 550.—O. Heer. On the Miocene Plants disco-
vered on the Mackenzie River, 560.
: Vol. xxxi. Nos. 206-212. 1880-81.
C. Schroter. Note on the Microscopic Examination of some fossil
Wood from the Mackenzie River, 147.—J. W. Hulke. Polacanthus Foxit,
a large undescribed Dinosaur from the Wealden Formation in the Isle of
Wight, 336.—R. Owen. Description of some Remains of the Gigantic
Land-lizard (Megalania prisca, Owen) from Australia, 380.—W. B. Pauli.
Notes on the Earthquakes of Julv 1880 at Manila, 460.—S. Haughton.
Notes on Physical Geology, No. 7. On the Secular Inequalities in Ter-
restrial Climates depending on the Perihelion, Longitude, and Eccentricity
of the Earth’s Orbit, 473.
Rugby-School Natural-History Society. Report for the year 1880.
1881.
EK. H. Acton. Subdivisions of the Carboniferous Limestone in Den-
bighshire, North Wales, 4.—A. Percy Smith. Holyhead, 20.—Seabroke.
The ‘Model’ (of the neighbourhood), 24—H. Y. Oldham. On some
Sections lately exposed near Rugby, 39.—T. K. Worthington. Report of
the Geological Section, 48.
St. Petersburg. Académie Imperiale des Sciences. Bulletin.
Tome xxvi. Nos. 2 & 3. 1880.
F, A. Forel. Les échantillons de limon dragués en 1879 dans les lac
d’ Arménie, 571.
: 4 Tome xxvii. Nos. 1&2. 1881.
N. v. Kokscharow. Beryll-Krystalle eines neuen Fundortes, 35.
: . Mémoires. Tome xxvil. Nos. 2-14. 1879-80.
J. Schmalhausen. LBeitrage zur Jura-Flora Russlands, No. 4.—V. vy.
Moller. Die Foraminiferen des russischen Kohlenkalks, No. 5.—L. v.
Schrenck. Der erste Fund einer Leiche von Rhinoceros Merchi, Jag., No.
7.—O. Heer. Nachtrage zur Jura-Flora Sibiriens, No. 10.
——. ——. ——. Tome xxviii. Nos.1 & 2. 1880.
Sanitary Institute of Great Britain. Transactions. Vol.i. 1880.
G. F. Symons. Address to Section 3, 173.—A. Haviland. Geology
in relation to Sanitary Science, 190.—J. Lucas. On the Quantitative
Elements in Hydrogeology, 195.—W. B. Kinsey. Particulars of an Ar-
tesian Well at Thames Haven, Essex, 203.—W. F. Stanley. Conditions
of the Water Supply of Croydon in relation to its Rainfall and Geology,
with Suggestions for its Sanitary and profitable Improvement, 225.
Scientific Roll and Magazine of Systematized Notes. Nos. 1-3.
1830-81. .
Shanghai. North-China Branch of the Royal Asiatic Society.
Journal. Vol.i. No.3. 1859.
._——. By Oly ails, INO: Iho eG:
W. H. Shock. Notes on the Mineral Resources of Japan, 92.
NeS aiNo 9s Sijos
—. 1. ——. ——. No. 12. 1878.
—. #——. —. —. No. 13. 1879.
—. «——. ——. —. No. 14. 1879.
ADDITIONS TO THE LIBRARY. 281
Sherborne. Dorset Natural-History and Antiquarian Field Club.
Proceedings. Vol.in. 1879.
J.C. Mansel-Pleydell. Anniversary Address of the President, 1.—A.
U. Kent. The finding Yerebratula Morierei at Bradford Abbas, 39.—J.
F,. Walker. The Occurrence of Terebratula Morieret in England, 42.—J.
C. Mansel-Pleydell. On the Dorset Trigone, 111.—J. Buckman. On
.a Series of Sinistral Gasteropods, 185.—J. Buckman. On the Belemno-
teuthis Montefiore, 141.
Society of Arts. Journal. .Vol. xxvii. Nos. 1440-146
C. G. W. Lock. Pandermite: a new Boracic Mineral, 76
: . Vol. xxix. Nos. 1461-1491. 1880-81. .
B. Latham. Croydon Bourne Flow, 84.—Hyde Clarke. Goldin India,
244.—Gold-mining in Japan, 286.—E. Whymper. Ascent of Chimborazo
and Cotopaxi, 353.—James Tennant, 366.—Marble Quarries of Algeria,
1880.
y
he
Society of Biblical Archeology. ‘Transactions. Vol. vii. Part 1.
1880.
Society of Medical Officers of Health. Annual Report 1878-79.
1879. Presented by W. Whitaker, Esq., F.GS.
——. Transactions. Session 1880-81. 1880. Presented by W.
Whataker, Esq., F.GS.
Stuttgart. Neues Jahrbuch fiir Mineralogie, Geologie und Palion-
tologie. 1879, Hefte 8 and 9. 1879.
A. Losch. Ueber Kalkeisengranat (Demantoid) von Syssertsk am
Ural, 785.— F. M. Stapff. Zur Mechanik der Schichtenfaltungen, 792.—
L. van Werveke. Beitrag zur Kenntniss der Gesteine der Insel Palma,
815.—F. Wohler. Bemerkungen itber das gronlandische Gediegen-Hisen,
832. S.M. Babcock. Ueber den Colestin aus dem Muschelkalke von
Juhbnde bei Gottingen, 835.—P. Herter. Ueber die Silicatgesteine im
EKocangebirge yon Massa maritima, 839.—C.A.Tenne. Ueber Hpistilbit,
840,—O. Schmidt. Bemerkungen zu “ Osc. Schmidt, Die Spongien des
Meerbusens von Mexico,” 841.—A. Arzruni. Cerithiwm corallense (Bu-
vignier) von Salatau, 842.—U. Stulz. Geologische Notizen aus den Alpen.
Ueber das Erstfelder Thal, 842.—K. Martin. Ueber das Tertiar von Java,
3800.—R. Richter. Diluvium bei Saalfeld, 850.—G. Berendt. Riesen-
kessel auf dem Riidersdorfer Muschelkalk bei Berlin, 351.—C. Struckmann.
Sowerbya Dukei in hannover’schen Pteroceras-Schichten, 853.—H. Fischer.
Ueber die Bezeichnung yon Farbenabstufungen bei Mineralien, 854.—T.
Fuchs. Ueber Solfataren in Serpentinstocken bei Kalamaki, 857.—E.
Cohen. Kersantit von Laveline. 858.—C. W. Giimbel. Vulkanische
Asche des Aetna von 1879, 859.—E. Cohen. Ueber einen Hklogit,
welcher als Hinschluss in den Diamanteruben von Jagersfontein, Grange
Freistaat, Std-Afrika vorkommt, 864.
é ») 18380) Bandi, 1380.
KE. Kalkowsky. Ueber die Erforschung der archaischen Formationem,
1.—H. Kalkowsky. Ueber Gueiss und Granit des bojischen Gneisstock-
werkes im Oberpfalzer Waldgebirge, 29.—C. A. Tenne. Ueber den Epi-
stilbit, 43.—F. Klocke. Ueber Doppelbrechung regularer Crystalle,
52.—F. Zirkel. Ueber den Zirkon als mikroskopischer Gesteins-
emengtheil, 80.—E. Dathe. Gletscherschliffe bei Lommatzsch in
achsen, 92.—A. Sauer. Titanmineralien in Amphiboliten, 94.—von
Konen. Tertiar zwischen Guntershausen und Marburg, 95.—H. Cohen.
Mandelstein aus den Maluti-Bergen, 96.—A. Inostranzeff. Ein neues
282 ADDITIONS TO THE LIBRARY.
ausserstes Glied in der Reihe der amorphen Kohlenstoffe, 97.—C. Struck-
mann. Vorlaufige Nachricht uber das Vorkommen erosser vogelahnlicher
Thierfahrten (Ornithoidichnites) im Hastingssandsteine von Bad Rehburg
bei Hannover, 125.—G. Seligmann. Krystallographische Notizen L, 129.
A. Weisbach. Zur Keuntniss des Leucits, 143.—G. Steinmann. Die Mu-
mien des Hauptrogensteins, 151—C. Klein. Ueber Goldstufen von
Vorospatak, 155.—A. Cossa. Rutil in Gastaldit-Eklogit von Val Tour- .
nanche, 162.—-A. Kenngott. Ueber Topas, Pyrrhotin und Pseudobrookit,
164.—H. Kayser. Ueber Barrande’s Brachiopodenwerk, 166.—A. Pichler.
Beitrage zur Geognosie Tirols, 172.—H. Fischer. Ueber Jadeit, 174.—F.
Schalch. Die Gliederung der Liasformation des Donau-Rheinzugs, 177.—
Des Cloiseaux. Ueber Pyrenien-Mineralien, 267.—T. Wolf. Geolovische
Arbeiten im Staate Ecuador, 268.—O. Fraas. Glaciales, 268.—Val. von
Moller. Schadel von Elasmotherium Fischert, Desm., 273.—G. vom Rath.
Contactverhaltnisse zwischen Kohle und einem basischen Eruptivgestein
bei Funfkirchen, 274.—A. Kenngott. Ueber Barytplagioklas, 278.—A.
Sauer. Rutil als mikroskopischer Gesteinsgemengtheil, 279.—-C. Klein.
Erwiderung, 281.—A. Koch. Ueber das Tertiar in Siebenbiirgen, 283.—
C. A. Tenne. Ueber ein neues Vorkommen von Epistilbit, 285.—C.
Klein. Berichtigung, 286.—E. Hussak. Eruptivgesteine von Schemnitz,
Augitandesit von St. Heidi, 287.
Stuttgart. Neues Jahrbuch fir Mineralogie, Geologie und Palion-
tologie. 1880, Bandu. Hefte 1-3. 1880.
C. E. Weiss. Die Krystallisationsgesetze seit C.S. Weiss, insbesondere
die Lehre von den Hemiédrieen, erlautert am Diamant, 1.—E. Cohen.
Ueber Laven von Hawaii und einigen anderen Inseln des grossen Oceans
nebst einigen Bemerkungen iiber glasige Gesteine im Allgemeinen, 23.—
M. Bauer. Beitrage zur Mineralogie. I. Reihe, 63.—A. Streng. Ueber
die Hinschlusse von Pflanzenresten in dem Hisensteinslager am Dunst-
berge bei Giessen, 83.—H. R. Goppert. Ueber die versteinerten Holzer
des Kytffhauser, 89.—A. Nehring. Ueber Fossilreste von Lemmingen,
93.—Herbich. Geologisches aus Bosnien und der Hercegowina, 94.—
H. H. Reusch. Die Alaunschieferscholle von Bikkelaget bei Christiania,
96.—F. Klocke. Ueber ein optisch anomales Verhalten des unterschwe-
felsauren Blei, 97.—O. Lang. Giebt es Gletscherspuren im Harz ?, 99.—
A. Stelzner. Bemerkungen tiber krystallinische Schiefergesteine aus
Lappland und iiber einen Augit-fithrenden Gneiss aus Schweden, 102.—
A. Streng. Erklirung, 107.—A. Weisbach. Mineralovische Notizen L.,
109.—F. Romer. Notiz tiber Belemnites ambiguus, Morton, aus der
Kreide von New Jersey, 115.—A. Nehring. Ein Spermophilus-Skelet
aus dem Diluvium des Galgenberges bei Jena, 118.—G. Steinmann. Zur
Kenntniss fossiler Kalkalgen (Siphoneen), 130.—L. van Werveke. Ueber
den Nephelin-Syenit der Serra de Monchique im stidlichen Portugal und
die denselben durchsetzenden Gesteine, 141.—W. OC. Brogger. Ueber
Olivinfels yon Sondmore, 187.—G. H. F. Ulrich. Mineralogisches aus
Neu-Seeland, 192.—A. Baltzer. Ueber Bergstiirze, 197.—F. Sandberger.
Sycidien aus dem Devon am Sjass, 199.—O. Liidecke. Ueber Skolezit,
Mesolith und Reissit, 200.—H. Fischer. Sprachliches zu Mineralogie
und Geologie, 203.—V. Goldschmidt. Unterscheidung von Arsenkies
und Arsenikalkies vor dem Lothrohr, 205.—H.:Rosenbusch. Glimmer-
trachyt von Montecatini in Toscana, 206.—C. Klein. Mineralogische
Mittheilungen VIT. 18. Ueber den Boracit, 209.—L. van Wervele. Mine-
ralogisch-petrographische Mittheilungen, 264.—W. Giimbel. Aus den
Alpen, 286.—F’. Sandberger. Ueber Nakrit von Siebenlehn; Pseudomor-
phosen von Gilbertit nach Zinnwaldit; Rotheisen nach Manganit; Stib-
lith nach Antimonit; Ehlit von Moldawa, 288.—O. Lang. Die Alaun-
ADDITIONS TO THE LIBRARY. 283
schieferscholle yon Biakkelaget, 290.—A. Pichler. Aus Tirol, 292.—O.
Miigge. Glimmerporphyrit vom Steinacher Joch, 293.—A. Koch. Ueber
siebenbiirgisches Tertiaér, 294.—A. Wichmann. Turmalin als authigener
Gemengtheil von Sanden, 294.—A. Nehring. Neue Notizen iiber fossile
Lemminge. Jin Losslager bei Mariaspring unweit Gottingen, 297.
Stuttgart. Neues Jahrbuch fir Mineralogie, Geologie und Palion-
tologie. 1881, Bandi. Heft 1. 1881.
G. Werner. Mineralogische Mittheilungen, 1—F. Klocke. Ueber die
optische Structur des Gletschereises, 23.—G. Steinmann. Die Forami-
niferengattung Nummoloculina, n. g., 31.—H. von thering. Die Aptychen
als Beweismittel fiir die Dibranchiaten-Natur der Ammoniten, 44.—E.
Cohen. Sammlung von Mikrophotographien zur Veranschaulichung der
mikroskopischen Structur von Mineralien und Gesteinen, 93.—P. Merian.
Zur Gattung Graphularia, M.-Edw. & Haime, 96.—R. D. M. Verbeek.
Zur Geologie von Sumatra und Java, 96.—F. Berwerth. Kommt Nephrit -
in den Alpen vor ?, 99.
: Beilage-Band i. Heft 1. 1880.
F. Maurer. Palaontologische Studien im Gebiet des rheinischen Devon.
4, Der Kalk bei Greifenstein, 1—H. Fischer. Ueber die mineralogische
Bestimmung archaologischer Steinobjecte, 113.—A. Koch. Petrogra-
phische und tektonische Verhaltnisse des Syenitstockes von Ditro in
Ostsiebenbiirgen, 152.
——. Verein fir vaterlindische Naturkunde in Wurttemberg.
Jahreshefte. Jahrgang 26. 1880.
C. Dorn. Anwendung der gelegentlich der Tiibinger Wasserversor-
gung gewonnenen Hrfahrungen fir die Wasserversorgung von Stuttgart,
53.—O. Fraas. Langenprofil der neuen Bahnlinie Stuttgart-Freudenstadt,
61.—O. Hahn. Ueber das Eophyllum canadense aus dem Serpentinkalk
des Laurentian-Gneisses von Canada, 71.—Leuze. Ueber die Kalk-
spathe im Basalttuff des Owener Boller, 74.
Swansea. South-Wales Institute of Engineers. Proceedings.
Vol. xu. Nos. 1-4. 1880.
H. Cossham. Some of the geological Problems in the Bristol Coalfield,
84.—T. Joseph. Observations on the Clayband-Ironstone, or “ Mine,” of
the Northern Outcrop of the South-Wales Coal-field, 255.
Sydney. Linnean Society of New South Wales. Proceedings.
Vol. iv. Part 4. 1880.
C. Jenkins. On the Geology of Yass Plains, 404.—C. 8. Wilkinson.
Notes on the Abercrombie Caves, 460.
: : Oven Area e OOO:
J. EH. Tenison-Wood. On a Fossiliferous Bed at the Mouth of the
Endeavour River, 187.
Royal Society of New South Wales. Journal. Vol. xii.
13879. 1880.
J. Hector. On the Geological Formations of New Zealand compared
with those of Australia, 65.—C.S. Wilkinson. Notes on the Occurrence
of remarkable Boulders in the Hawkesbury Rocks, 105.
Taunton. Somersetshire Archeological and Natural-History Society.
Proceedings. Vol. xix. (1873). 1874. Presented by H. B.
Woodward, Esq., F.GLS.
H. B. Woodward. Notes on the Geology of the Neighbourhood of
Wells, Somerset, 50. |
284 ADDITIONS TO THE LIBRARY.
Tokio. University of. Memoirs of the Science Department. Vol. 1.
Part 1. 2539 [1879].
EH. 8. Morse. Shell-mounds of Omori, 1.
: : Noli 2539) (379):
C. Netto. Mining and Mines in Japan, 1.
—_—_———
. The Calendar of the Departments of Law, Science,
and Literature. 2539-40 [1879-80].
Troms6 Museums Aarshefter. Heft ii. 1880.
Karl Pettersen. Terrasser og gamle strandlinjer, 1—R. Collett.
Glaciale Mergelboller med indesluttede Fiskelevninger fra Bejeren 1
Salten, 96.
Turin. Osservatorio della Regia Universita. Bollettino. Anno xiy.
(1879). 1880.
—. —. —. Anno xy. (1880). 1881.
——. Reale Accademia delle Scienze. Atti. Vol. xv. Disp. 1-8.
1879-80.
A.Cossa. Sui cristalli microscopici di rutilo contenuti in una eclogite
di Val Tournanche, 21.—A. Portis. Intorno ad alcune impronte eoceniche
di vertebrati recentemente scoperte in Piemonte, 221.—G. Berruti e L.
Bellardi. Relazione sopra una memoria del Professore Martino Baretti,
intilolata: Il ghiacciaio del Miage, 299.—M. Baretti. Sui resti fossili
di Rinoceronte nel territorio di Dusino, circondario d’Asti, provincia
d’ Alessandria, 678, 751.—G. Spezia. Nota sul calcare albitifero dell’ Ar-
gentera (Cuneo), 785.
: 2 Vol. xvi. Disp. 1-5. 1881.
A. Cossa. Nota su alcune roccie sepentinose del Gottardo, 71.—G.
Berruti e M. Lessona. Relazione sulla memoria presentata dal Dottore
Alessandro Portis col titolo: Sui terreni stratificati di Argentera (Valle
di Stura), 199.—A. Cossa. Nota sopra alcune roccie serpentinose
dell’ Appennino bobbiese, 296.—A. Cossa e E. Mattirolo. Sopra alcune
roccie del periodo silurico nel territorio d’ Iglesias, Sardegna, 385.—
G. Piolti. Nota sopra alcune pietre a sccdelle dell Anfiteatro morenico
di Rivoli, Piemonte, 403.
University College. Calendar (Session 1880-81). 1880.
Victoria Institute. Journal of the Transactions. Vol. xiv. Nos.
A= jon lesOLell.
T. McK. Hughes. On the Evidence of the later Movements of Eleva-
tion and Depression in the British Isles, 248.
eS )6OWOL aa, INO, SSB IL
Vienna. Archiv fiir practische Geologie. Bandi. 13880.
F. Posepny. Die Goldbergbaue der Hohen Tauern mit besonderer
Beriicksichtigung des Rauriser Goldberges, 1—F’. PoSepny. Die Erzla-
gerstatten von Kitzbiihel in Tirol und der angrenzenden Theile Salzburgs,
257.—F. PoSepny. Die Erzlagerstatten am Pfundererberge bei Klausen
in Tirol, 441.—H. Hofer. Die Edelmetall-Production Karntens, 490.—
F. Pogepny. Ueber den alten Bergbau in Tirol, 520.—F. Posepny. Geo-
logie und Bergbau in ihren gegenseitigen Beziehungen, 531.
ADDITIONS TO THE LIBRARY. 285
Vienna. Beitraige zur Paliontologie von Oseterreich-Ungarn und den
angrenzenden Gebieten. Bandi. MHefte 1 & 2. 1880-81.
Purchased.
H. Zugmayer. Untersuchungen tiber rhatische Brachiopoden, 1.—A.
Bittner. Beitrage zur Kenntniss alttertiarer Hchinidenfaunen der Siid-
alpen, 43, 73.—V. Uhlig. Die Jurabildungen in der Umgebung von
Brunn, 111.
——. Kaiserliche Akademie der Wissenschaften. Anzeiger. 1880,
Nos. 11-16. 1880.
F. Toula. Geologische Untersuchung des westlichen Balkan, 86.—
J. Wold¥ich. Diluvialfauna von Zuzlawitz bei Winterbere im Bohmer-
walde, 89.
——, ——. ——. 1880, Nos. 20-28. 1880.
J.C. Labhart. Ueber die im Monate Juli d. J. [in Manila] stattge-
funden Erdbeben, 195.
: . ——. 1881, Nos. 7-13. 1881.
F. Toula. Grundlinien der Geologie des westlichen Balkan, 62.—A.
Brezina. Ueber die Meteoreisen von Bolson de Mapimi, 103.
: Denkschriften. Band xl. 1880.
A. Bittner. Der geologische Bau von Attika, Bootien, Lokris, und
Parnassis, 1—M. Neumayr. Der geologische Bau des westlichen Mittel-
Griechenland, 91.—Fr. Teller. Der geologische Bau der Insel Eubéa,
129.— Fr. Teller. Geologische Beschreibung der studoéstlichen Thessalien,
183.—M. Neumayr. Ueber den geologischen Bau der Insel Kos und
tiber die Gliederung der jungtertiaren Binnenablagerungen des Archipels,
213.—M. Neumayr. Geologische Beobachtungen im Gebiete des thes-
salischen Olymp, 315.—L. Biurgerstein. Geologische Untersuchungen
im sudwestlichen Theile der Halbinsel Chalkidike, 321.—M. Neumayr.
Geologische Untersuchungen uber den nordlichen und ostlichen Theil der
Halbinsel Chalkidike, 328.—F’. Teller. Geologische Beobachtungen auf
der Insel Chios, 340.—F’. Calvert und M. Neumayr. Die jungeren Abla-
gerungen am Hellespont, 857.—A. Bittner, M. Neumayr, und Fr. Teller.
Ueberblick tiber die geologischen Verhaltnisse eines Theiles der agaischen
Kustenlander, 379.
: . ——. Band xli. 1879.
T. Fuchs. Ueber die von Dr. E. Tietze aus Persien mitgebrachten
Tertiarversteinerungen, 99.—L. Szajnocha. Die Brachiopodon-Fauna
der Oolithe von Balin bei Krakau, 197.
; : Band xli. 1880.
Hofer. Die Erdbeben Karntens und deren Stosslinien, 1—Hornes.
Materialien zu einer Monographie der Gattung Megalodus mit besonderer
Beriicksichtigung der mesozoischen Formen. 91.—Manzoni. Kchino-
dermi fossili della molassa serpentinosa e supplemento agli Echinodermi
fossili dello schlier delle colline di Bologna, 185.
. Sitzungsberichte. Band lxxix. Hefte 1-5. 1879.
J. Niedzwiedzki. Geologische Untersuchungen im westlichen Theile
des Balkans und in den angrenzenden Gebieten zur Kenntniss der
Eruptivgesteine des westlichen Balkans, 139.—V.v. Zepharovich. Halo-
trichit und Melanterit von Idria, 183,—A. Boué. Ueber die Oro-Potamo-
Limne- (Seen) und Lekanegraphie (Becken) des Tertiaren der europaischer
Tirkei und Winke zur Ausfullung der Liicken unserer jetzigen geogra-
phischen und geognostischen Kenntnisse dieser Halbinsel, 26].—Liebe.
286 ADDITIONS TO THE LIBRARY.
Die fossile Fauna der Hohle Vypustek in Mihren nebst Bemerkungen
betreffs einiger Knochenreste aus der Kreuzberghohle in Krain, 472.
Vienna. Kaiserliche Akademie der Wissenschaften. Sitzungs-
berichte. Band Ixxx. Hefte 1-5. 1880.
J. V. Janovsky. Ueber Niobit und ein neues Titanat vom Isergebirge,
34,—J. Rumpf. Ueber den Krystallbau des Apophyllits, 84.—F. Becke.
Ueber die Zwillingsbildung und die optischen Kigenschaften des Chabasit,
90.—F. Berwerth. Ueber Nephrit aus Neu-Seeland, 102.—F. Berwerth.
Ueber Bowenit aus Neu-Seeland, 116.—M. Slabnetier. Ueber die optische
Orientirung der Plagioklase, 192. —V. Uhlig. Ueber die liasische Bra-
chiopodenfauna yon Sospirolo. bei Belluno, 259.—F. Hochstetter. Ergeb-
nisse der Hl plectiosel anita sien : im Jahre 1879, zweiter Bericht, 526.
ao SS Sin Io, Lele IES, S80,
T. Fuchs. Weber einige tertiaire Hchiniden aus og 97.—A. Boué,
Ueber den ehemaligen und jetzigen Stand der Geologie und Geogenie
und die Untersuchung en und Methoden in diesen Richtungen, 148.—Leo
Birgerstein und Franz Noé. Geologische Beobachtungen im sudlichen
Calabrien, 154.—F. Toula. Geologische Untersuchungen im westlichen
Theile des Balkan und in den angrenzenden Gebieten (1X.), 188.
Band Ixxxi. Hefte 1 & 2. 1880.
J. N. Woldfich. Diluviale Fauna von Zuzlawitz bei Winterberg im
Bohmerwalde, 7.—J. Sieber. Zur Kenntniss der nordbéhmischen Braun-
kohlenflora, 67.—V. Bieber. Ueber zwei neue Batrachier der bohmischen
_Braunkohlenformation, 102.—C. v. Ettingshausen. Beitrage zur Erfor-
schung der Phylogenie der Pflanzenarten, 133.—G. Tschermak und L.
Lipoez. Beitrag zur Kenntniss des Zoisits, 141.—K. Hussak. Beitrige
zur Kenntuiss der Er uptivgesteine der U mgegend von Schemnitz, 164.
——. Kaiserlich-konigliche Bergakademien zu Leoben und Pribram
und die konighch ungarischen Bergakademie zu Schemnitz.
Berg- und huttenminnisches Jahrbuch. Band xxviii. Hefte
2-4, 1880.
K. Reyer. Zinn in Cornwall, 153.
——. ——. ——. Band xxix. Heft 1. 1881.
HK. Reyer. Ueber die “‘Granitstocke,” 15.—H. Reyer. Was versteht
der Bergmann unter dem Worte “ Stock” 2, 20.—M. v. Lill, Analysen
ausgefiihrt im Laboratorium des k. k. General-Probiramtes in Wien im
Jahre 1880, 27,
Kaiserlich-konigliche geologische Reichsanstalt. Abhand-
lungen. Band xii. Heft 2. 1880.
R. Hornes und M. Auinger, Die Gasteropoden der Meeresablage-
rungen der ersten und zweiten miocinen Mediterranstufe in der dster-
reichisch-ungarischen Monarchie, I1., 53.
Jahrbuch. Band xxx. Hefte3 &4. 1880.
F. vy. Hauer. Grundlinien der Geologie von Bosnien-Hercegovina
(Vorwort), 160.—E. v. Mojsisovics. Grundlinien der Geologie von
Bosnien-Hercegovina. I. West-Bosnien und Turkisch-Croatien, 167.—
KE. Tietze. Grundlinien der Geologie von Bosnien-Hercegovina. II.
Das ostliche Bosnien, 266.—A. Bittner. Grundlinien der Geologie von
Bosnien-Hercegovina. III. Die Hercegovina und die sudostlichsten
Theile von Bosnien, 353.—C. v. John. Grundlinien der Geologie von
Bosnien- Hercegovina. IV. Ueber krystallinische Gesteine Bosnien’s und
der Hercegovina, 439.—M. Neumayr. Grundlinien der Geologie von
Bosnien-Hercegovina. V. Tertiire Binnenmollusken aus Bosnien und
ADDITIONS 10 THE LIBRARY. 2387
der Hercegovina, 465.—M. Vacek. Neocomstudie, 493,—I. Reyer. Die
Bewegung im Festen, 543.—KH. Kayser. Zur hercynischen Frage, 556.—
D. Kramberger. Die fossilen Fische von Wurzenege bei Prassberg in
Steiermark, 565.—V.v. Moller. Ueber einige Foraminiferen-fiihrenden
Gesteine Persien’s, 573.—M. Lomnicki. Die galizisch-podolische Hoch-
ebene zwischen dem oberen Laufe der Fliisse Gnila, Lipa und Strypa, 587.
—R. Scharizer. Mineralogische Beobachtungen, 593.—A. Cathrein. Die
Dolomitzone bei Brixlege in Nordtirol, 609.—H. Walter. Ein Durch-
schnitt in dem Mittelkarpathen von Chyréw tiber Uherce und den un-
garischen Grenzkamm bis Sturzica, mit Beriicksichtigung eniger Paral-
lel-durchschnitte, 635.—R. Hornes. Die Trilobiten-Gattungen Phacops
und Dalmamnites und ihr vermuthlicher genetischer Zusammenhang, 651.
—K.M. Paul. Ueber die Lagerungsverhiltnisse in Wieliczka, 687.—
HE. von Mojsisovics. Ueber heteropische Verhiltnisse im Triasgebiete
der lombardischen Alpen, 695.—J. Schmidt. Ueber die Fossilien des
Vincaberges bei Karlstadt in Croatien, 719.—E. Tietze. Zur Geologie der
Karsterscheinungen, 729.
Vienna. Kaiserlich-konigliche geologische Reichsanstalt. Jahr-
bouche Band xxxi. Nov. 13881.
HE. Reyer. Predazzo, 1.—H. Reyer. Ueber Tuffe und tuffogene Sedi-
mente, 5/.—E. Tietze. Ueber einige Bildungen der jiingeren Epochen
in Nord-Persien, 67.—C. M. Paul. Die Petroleum- und Ozokerit-Vor-
kommnisse Galiziens, 131.
. ——. Verhandlungen. 1880, Nos. 10 and 11. 1880.
A. Heim. Ueber die Glarner Doppel-Falte, 156.—R. Hornes. Mas-
todon angustidens von Oberdorf nordlich von Weiz, 159.—V. Bieber.
Ueber zwei neue Batrachier aus dem Diatomaceenschiefer bei Sulloditz
in Bohmen, 160.—E. Hussak. Ueber Eruptivgesteine von Gleichenberg,
160.—T. Fuchs. Ueber ein neues Vorkommen von Stisswasserkalk bei
Czeikowitz in Mahren, 162.--R. Hornes. Tertiar bei Derwent in
Bosnien, 164.—E. Suess. Ueber die vermeintlichen saécularen Schwan-
kungen einzelner Theile der Erdoberflache, 171.—C. von Hauer. Krys-
tallogenetische Beobachtungen, 181.—M. Vacek. Hrwiederung auf die
Mittheilung des Herrn Prof. A. Heim in Nr. 10 der Verhandlungen, 189.—
R. Hornes. Die Stosslinie des Villacher Erdbebens von 1348, 193.—R.
Hornes. Amphiope nov. sp. vom Seckauer Berg bei Leibnitz, 194.
é ——. 1880, Nos. 13-17. 1880.
Karl Ritter von Hauer, 229.—H. Reyer. Ueber die Tektonik der gra-
nitischen Gesteine von Predazzo, 231.—A. Bittner. Die Sedimentgebilde
in Judicarien, 253.—V. Hilber. Reisebericht aus Ostgalizien, 238.—
R. Hornes. Das Auftreten der Gattung Terebra in den Ablagerungen
der ersten und zweiten miocainen Mediterran-Stufe der 6sterreichisch-
ungarischen Monarchie, 245.—W. Jicinsky. Basalt in der Jaklowetzer
Grube bei Mahr.-Ostrau, 247.—G. Stache. Durchschnitt durch die krys-
tallinische Centralmasse und die palaolithischen Randzonen der Alpen
vom Gailthaler Gebirge uber das Tauernkreuzjoch nach dem Innthal bei
Woregl, 249.—G. Stache. Der krystallinische Gebirgs-Abschnitt zwischen
dem hinteren Ulten-Gebiet und Unter-Sulzberg, 250.—G. Stache. Aus
den Randgebieten des Adamellogebirges, 252.—E. Tietze. Die Gegend
von Rospucie in Galizien, 255.—F. Teller. Verbreitung und Lagerung
der Diorite in der Umgebung von Klausen und Liisen, 261.—V. Hilber.
Reiseberichte aus Ostgalizien, 264.—R. Hornes. Das Erdbeben vom
9. November in Steiermark, 269.—M. Lomnicki. LEiniges tiber die Gyps-
formation in Ostgalizien, 272.—V. Uhlig. Zur Gliederung des rothen
Ammonitenkalkes in der Umgebung von Roveredo, 275.—C. W. Gumbel.
288 ADDITIONS TO THE LIBRARY.
Rothkalk. Magnesit von Elmen, 276.—G. C. Laube. Pflanzenreste aus
dem Diatemaceenschiefer in Sulloditz im bohm. Mitteleebirge, 277.—
G. Starke. Notizen uber Bol und Polyhydrit, 278.—KH. Tietze. Zur
Geologie der Karsterscheinungen, 281.—F’. y. Hauer. Bouteillenstein von
Trebitsch, 282.—J. N. Woldrich. Beitrage zur diluvialen Fauna der
mihrischen Hohlen, 284.—G. Stache. Ueber das Vorkommen von
Olivingesteinen in Stidtirol, 287.—E. Reyer. Die Resultate eines Ver-
suches tiber Bewegung im Festen, 288.—D. Kramberger. Die jung-
tertiare Fischfauna Croatiens, 297.—A. Rzehak. Ueber die Gliederung
und Verbreitung der alteren Mediterranstufe in der Umgebung von Gr.
Seelowitz in Mahren, 300.—F. Teller. Vorlage des Blattes Klausen, 303.
—E. Reyer. Ueber Predazzo, 304.—L. Szajnocha. Vorlage der geolo- -
gischen Karte der Gegend von Gorlice, 304.—A. Biezina. Ueber ein
neues Mineral, den Schneebergit, 313.—K. Hussak. Umeeschmolzene
Basalte und Granite von Hdersertin bei Karlsbad, 314.—J. Kusta. Zur
Geologie und Palaontologie des Rakonitzer Steinkohlen-Beckens, 317.—
G. Sebisanovic. Hiniges tiber die Erdbeben von Karlstadt in Kroatien,
325.—R. Hornes. Vorlage emer geologischen (Manuscript-) Karte der
Umgebung von Graz, 326.—H. von Mojsisovics. Ueber heteropische
Verhaltnisse im Triasgebiete der lombardischen Alpen, 330.—C. M. Paul.
Geologische Karte der Gegend von Przemysl, 380.
Vienna. Kaiserlich-kénigliche geologische Reichsanstalt. Verhand-
lungen. 1881, Nos. 1-11. 1881.
Fr. Ritter v. Hauer. Jahresbericht, 1—M. v. Hantken. Arbeiten
der k. ungarischen geologischen Anstalt, 15.—v. Loeffelholz. Hinige
geognostische Notizen aus Bosnien, 23.—A. Bittner. Bemerkungen zu
voranstehender Mittheilung, 27.—F. Kreutz. Ueber den Ursprung des
Erdols in der galizischen Salzformation, 28.—EH. Tietze. Das Alter des
Kalkes von Steinbergen bei Graz, 34.—G. Stache. Ueber die Gesteine
des Adamello-Gebirges, 37.—EH. Tietze. Ueber die geologische Aufnahme
der Gegend von Lemberg und Grodek, insbesondere tiber den Loss dieser
Gegend, 37.—M. Vatek. Ueber die Schichtenfolge in der Gegend der
Glarner Doppelfalte, 48.—V. Uhlig. Zur Kenntniss der Malm- und
Tithonstufe in der Umgebung von Steierdorf im Banat, 51.—A. Bittner.
Mittheilungen aus dem Aufnahmsterrain, 52.—D. Stur. Gebirgshub
und Gebirgsschub, 58.—EH. Tietze. Bemerkungen zu den Ansichten
von F, Kreutz uber das Erdol der galizischen Salzformation, 59,—
E. v. Mojsisovics. Zur Karstgeologie, 65.—S. Kontkiewicz. Kurzer
Bericht uber die von ihm ausgefuhrten geologischen Untersuchungen
im stidwestlichen Theile vom Konigreich Polen, 66.—F. Teller. Zur
Tektonik der Brixener Granitmasse und ihrer nordlichen Umrandung,
69.—E. Reyer. Ueber die Tuffe der massigen Euptivgesteine, 74.—T.
Fuchs. Chalicotheriwm von Siebenhirten, 77.—-A. Rzehak. Die Fauna
des mihrischen Rothliegenden, 78.—C. Dolter. Von den capverdischen
Inseln, 79.—v. Lorenz. Ueber terra rossa, 81.—H. von Dunikowski.
Geologische Verhaltnisse der Dniesterufer in Podolien, 82.—H. Reyer.
Ueber Predazzo, 85.—v. Loffelholz. Hin Beitrag zur Feststellung des
Alters der Lossbildung bei Wien, 89.—J. Wentzel. Fossile Pflanzen aus
den Basalttuffen von Warnsdorf in Bohmen, 90.—G. Laube. Neue
Knochenfiinde aus dem Lehm der Umgebung von Prag, 93.—C. M. Paul.
Ueber Petroleumvorkommnisse in der nordlichen Walachei, 93.—V.
Hilber. Vorlage geologischer Karten aus Ost-galizien, 95.—F. Kreutz.
Erklarung zu Dr. Tietze’s ‘‘ Bemerkungen zu den Ansichten von F. Kreutz
uber das Hrdol der galizischen Salzformation, 101.—E. Kittl. Ueber einen
neuen Fund von Listrzodon, 103.—H. v. Mojsisovics. Ueber die Cephalo-
podon-Fauna der Trias-Schichten von Mora d’Ebro in Spanien, 105,—
ADDITIONS TO THE LIBRARY. 289
K. M. Paul. Ueber das Ozokerit- und Erdél-vorkommen von Boryslaw,
107.—F. Kreutz. Ueber die Bildung und Umbildung von E rdwachs und
Erdél in Galizien, 115.—F. Puen: “Ucher den Ursprung des Steinsalzes
am Rande der Karpathen, a. Pseudometeorit, gefunden
in Cista, Pilsener Kreis, A. H. Schindler. Neue Angaben
liber die Mineralreichthiimer Bees und Notizen tiber die Gegend
westlich von Zendjan, 122 2.—V. Hilber. Die Stellung des oste: alizischen
Gypses und sein V erhiltniss zum Schlier, 123.—H. y. Foullon. Krys-
tallogenetische Beobachtungen, 131.—H. Kittl. Ueber die Mineralquellen
Nordbéhmens, 149.—F. Wurm. Limonitconecretionen in der Umgebung
von Béhmisch-Leipa, 153.—H. Engelhardt. Dritter Beitrag zur icennt.
niss der Flora des Thones von Preschen bei Bilin, 154.—D. ‘Kramberg er.
Studien tiber die Gattung Sawocephalus, 155.—W. Dames. Ueber “die
Cephalopoden aus dem Gaultquader des Hoppelberges, 155.—C. Dolter.
Spuren eines alten Festlandes auf den capverdischen Inseln, 156.—M.
Vacek. Vorlage der geologischen Karte der Umgebung von Trient, 157.
—L. Szaynocha. Das “Petroleumvorkommen von Sloboda rungur ska, 162.
Vienna. Kaiserlich-kénigliche zoologisch-botanische Gesellschaft.
Verhandlungen, 1880. Band xxx. 1881.
—. Mineralogische und petrographische Mittheilungen. Neue
Folge. Bandi. Hefte 1-6. 1880-81. Purchased.
Curt von Eckenbrecher. Untersuchungen tber Umwandlungsvorgange
in Nephelingesteinen, 1.—C. W. C. Fuchs. Die vulkanischen Hreignisse
des Jahres 1879,35.—J. Becke. Hypersthen von Bodenmais, 60.—A.
Penck. Die pyroxenfiihrenden Gesteine des nordsachsischen Porphyrge-
bietes, 71.—P. Jannasch und J. H. Kloos. Mittheilungen tiber die laystal-
linischen Gesteine des Columbia Flusse in Nordamerika und die darin
enthaltenen Feldspathe, 97—Max Schuster. Ueber die optische Ori-
entirune der Plagioklase, 117.—A. Frenzl. Mineralogisches aus dem
ostindischen Archipel, 289.—F. Becke. Ueber den Hessit (Tellursil-
berglanz) von Botes in Siebenburgen, 301.—G. Tschermak. Der Boden
und die Quellen von Slanik, A Ja Pohlig. Die een ce
im Siebenbirger Trachyt von der Perlenkardt bei ae <0. W.
Cross. Studien iiber bretonische Gesteine, 369.—G. ‘Stein Die
Melaphyre der kleinen Karpathen, 411.—H. Dietrich. ee Unter-
suchung der drei neuen Mineralquellen von Krynica, 439.—J. Blaas.
Petrographische Studien an jiingeren Eruptivgesteinen Persiens, 457.—
A. Frenzel. Mineralogisches, 504.—A. v. Lasaulx. Ueber sogenannten
kosmischen Staub, 517.—K. Geinitz. Der Phyllit von Rimognes in den
Ardennen, 533.
Washington. Smithsonian Institution. Annual Report of the Board
of Regents for 1878. 1879.
——, ——. Annual Report of the Board of Regents for 1879.
1880.
W. Gesner. Mica Beds in Alabama, 382.
——. ——. Contributions to Knowledge. Vol. xxii. 1880.
-——, ——. Miscellaneous Collections. Vol. xvi. 1880.
——. ——. Vol. xvi. 1880.
Watford Natural-History Society and Hertfordshire Field-Club.
Transactions. Vol. ii. Part 8. 1880.
VOL. XXXVII. y
290 ADDITIONS TO THE LIBRARY.
Watford. Hertfordshire Natural-History Society and Field-Club.
Transactions. Vol.i. Parts 1-4. 1880-81.
J. Gwyn Jeffreys. Anniversary Address, 84.—H. Gilbertson. Notes .
on Sponges, recent and fossil, 97.—J. V. Elsden. The Post-Tertiary
Deposits of Hertfordshire, 1053. r
Wellington, N. Z. New-Zealand Institute. Transactions and Pro-
ceedings. Vol. xii. (1879). 1880.
W. Colenso. On the Moa, 63.—J. C. Crawford. On Wind-formed
Lakes, 415.—J.C. Crawford. On Bidwill’s Front Hills, 416.—W. Collie.
Remarks on Volcanoes and Geysers of New Zealand, 418.
Wiesbaden. Nassauische Vereins fiir Naturkunde. Jahrbiicher.
Jahrgang 31 u. 32 (1878 u. 1879). 1880.
R. Fresenius. Chemische Analyse der Mineral-Quelle bei Biskirchen
im Lahnthale, 1—R. Fresenius. Analyse der Wappen-Quelle zu Bad
Ems, 17.—R. Fresenius. Analyse des Kaiser-Brunnens zu Bad Ems,
32.—R. Fresenius. Chemische Untersuchung der warmen Quelle zu
Schlangenbad, 49.—R. Fresenius. Chemische Analyse der Wilhelms-
Quelle zu Kronthal, 70.—Fr. Wenckenbach. Uebersicht tiber die in
Nassau aufgefundenen einfachen Mineralien, 147.
- York. Natural-History Journal. Vol. iii. Nos. 3,4,6&7. 1879.
Presented by W. Whitaker, Esq., F.G.S.
J. EK. Clark. ae Bog I., 115.
—. —-. Vol. Cee 23-31. 1880. Presented by W.
Whitaker, Esq., r. G. Se
J.P. Drewett. St. Bee’s Head, 11, 24.
—. Yorkshire Philosophical Society. Annual Report for 1880.
1880.
T. S. Noble. An Account of the Scientific Work of Prof. HK. E.
Deslongchamps, 53.—T. 8. Noble. M. J. Barrande and the Darwinian
Theory of Evolution, 54.
Zoological Society. Proceedings. 1880, Parts 2-4. 1880-81.
T. H. Huxley. On the Application of the Laws of Evolution to the
Arrangement of the Vertebrata, and more particularly of the Mammalia,
649.
———, | ssi Part esis
——, Transactions. Vol: x1. Parts 2—5) 1Ss0=cie
2. Booxs.
Names of Donors in Italics.
Achepohl, L. Das niederrheinisch-westfalische Steinkohlengebirge.
Atlas der fossilen Fauna und Flora. Lieferung1&2. Fol. Essen,
1880-81. Purchased.
Achiardi, A.@. Su di alcuni minerali della miniera del Frigido
presso Massa nelle Alpi apuane. 8vo. Pisa, 1881.
Angelin, N. P. Paleontologia Scandinavica. P. 1. Crustacea
formationis transitionis. Fasc.1 &11*. 4to. Stockholm, 1878.
Presented by the Royal Academy of Scrences, Stockholm.
ADDITIONS TO THE LIBRARY. 291
Angelin, N. P., et G. Lindstrém. Fragmenta silurica e dono Caroli
Henrici Wegelin. Fol. Stockholm, 1880. Presented by the Royal
Academy of Stockholm.
Anon, Canada: a Hand-book of Information for intending Emi-
grants. 8vo. Ottawa, 1879. Presented by W. Whitaker, Esq.,
HGS.
—. Notes on the Geology of Ilfracombe and its Neighbourhood
by a late Resident. 12mo. Ilfracombe, 1880.
——. Scepticism in Geology and the Reasons for it, by Verifier.
2nd edition. 8vo. London, 1878. Presented by Prof. P. M.
Duncan, F.BRS., F.GS.
Ansted, D. T. A short Trip in Hungary and Transylvania in the
Spring of 1862. 8vo. London, 1862. Purchased.
Water and Water-supply, chiefly in reference to the British
Islands. 8vo. London, 1878. Purchased.
Atkinson, E. T. Economic Mineralogy of the Himalayan Districts
of the North-western Provinces. 8vo. Calcutta, 1881.
Attwood, G. A Contribution to South-American Geology. With an
Appendix by the Rev. Prof. 7. G. Bonney. 8vo. London, 1879.
Attwood, G. Practical Blowpipe Assaying. 8vo. London, 1880.
Ball, V. On Spheroidal Jointing in Metamorphic Rocks in India
and elsewhere, producing a structure resembling glacial ‘ Roches
Moutonnées.” 8vo. Dublin, 1880.
. On the Coal-fields and Coal-production of India. 8vo.
Dublin, 1880.
On the Evidence in favour of the Belief in the Existence of
floating Ice in India during the Deposition of the Talchir
(Permian or Permio-Triassic) Rocks. 8vo. Dublin, 1880.
. On the Mode of Occurrence and Distribution of Gold in
India. 8vo. Dublin, 1880.
Barrande, J. Du maintien de la nomenclature établie par M.
Murchison. 8vo. Paris, 1880.
Barrois, C. Note on the Rey. J. F. Blake’s paper on the Chalk of.
Yorkshire. 8vo. London, 1880.
——. Note sur les alluvions de la Serre (Aisne). 8vo. Lille,
1880.
Sur le terrain silurien supérieur de la presqwile de Crozon.
8vo. Lille, 1880.
. Sur quelques espéces nouvelles ou peu connues du terrain
erétacé du Nord de la France. 8vo. Lille, 1880.
Baverman, Hilary. Text-book of Systematic Mineralogy. 8vo..
London, 1881.
y 2
292 ADDITIONS TO THE LIBRARY.
Belgium. Commnussion de la Carte Géologique de la Belgique. Texte
explicatif du levé géologique de la planchette d’Aerschot, par M. le
baron O. van Ertborn, avec la collaboration de P. Cogels. 8vo.
Brussels, 1880.
Texte explicatif du levé géologique de la planchette
@ Anvers, par M. le baron O. van Ertborn, avec la collaboration
de P. Cogels. 8vo. Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Beveren, par M. le baron O. van Ertborn et P. Cogels. 8vo.
Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Boisschot, par M. le baron O. van Ertborn et P. Cogels. 8vo.
Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Boom, par M. le baron O. van Ertborn, avec la collaboration de
P. Cogels. S8vo. Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Heyst-op-den-berg, par M. le baron O. van Ertborn, avec la
collaboration de M. P. Cogels. 8vo. Brussels, 1880.
; Texte explicatif du levé géologique de la planchette
de Lierre, par M. le baron O. van Ertborn, avec la collaboration
de M. P. Cogels. S8vo. Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Lubbeek, par M. le baron O. van Ertborn et P. Cogels. 8vo.
Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de “Malines, par M. le baron O. van Ertborn et P. Cogels. 8vo.
Brussels, 1880.
Texte explicatif du levé géologique de la planchette
de Putte, par M. le baron O. van Ertborn, avec la colloboration
de M. P. Cogels. 8vo. Brussels, 1880.
Benecke, E. W., und E. Cohen. Geognostische Beschreibung der
Umgegend von Heidelberg. Hefte 2 & 3. 8vo. Strassburg,
1880-81. °
Binney, HE. W. On some Marine fossil Shells in the Middle Coal
Measures of Lancashire. S8vo. Manchester, 1880.
Bittner, A., L. Burgerstein, F. Calvert, Fr. Heger, V. Hilber, 1.
Neumayr und Fr. Teller. Geologische Studien in den Kusten-
landern des griechischen Archipels. 4to. Vienna, 1880.
Blake, J. H. Address at the Anniversary Meeting of the Norwich
Geological Society, 2nd November 1880. 8vo. Norwich, 18381.
Blake, W. P. Report of a Geological Reconnaissance in California,
made in connexion with the Expedition to survey Routes in
California to connect with the surveys of routes for a Railroad
from the Mississippi River to the Pacific Ocean, under the com-
ADDITIONS TO THE LIBRARY. 293
mand of Lieut. R. 8. Williamson. With an Appendix containing
descriptions of portions of the collection by Louis Agassiz, A. A.
Gould, J. W. Bailey, T. A. Conrad, John Torrey, G. C. Schaeffer,
and J. D. Haster. 4to. New York, 1858. Purchased.
Bohemia. Naturwissenschaftliche Landesdurchforschung yon Boh-
men. Archiv, Band LV. No. 2(1880). Erliuterungen zur geolo-
gischen Karte der Umgebungen von Prag, yon J. Krejci und
R. Helmhacker. 8vo. Prague, 1880. Purchased.
Bonney, T.G. Note on a Case of Prismatic Structure in Ice. 8vo.
On Traces of Glacial Action near Llandudno. 8yvo. London,
1867.
—. On supposed Pholas Burrows in Derbyshire. 8vo. London,
1870.
——. Ona Cirque in the Syenite Hills of Skye. 8vo. London,
ixey al
——. On the Formation of ‘“ Cirques,” and their Bearing upon
Theories attributing the Excayation of Alpine Valleys mainly to
the Action of Glaciers. 8vo. London, 1871.
Ice Scratches in Derbyshire. 8vo. London, 1872.
On certain Lithodomous Perforations in Derbyshire. 8vo.
London, 1872.
Notes on the Roslyn-Hill Clay-pit. 8vo. London, 1872.
Lakes of the North-eastern Alps and their Bearing on the
Glacier-Erosion Theory. 8vo. London, 1873.
On the Occurrence of a Quartzite Boulder in a Coal-seam in
South Staffordshire. 8vyo. London, 1873.
——. Some Notes on Glaciers. 8vo. London, 1876.
—. OnColumnar, Fissile, and SpheroidalStructure. 8vo. London,
1876.
On certain Rock-structures, as illustrated by Pitchstones
and Felsites in Arran. 8yo. London, 1877.
On Mr. Helland’s Theory of the Formation of Cirques. 8vo.
London, 1877.
. On the Microscopic Structure of Luxullianite. 8vo. Truro,
hove
On the Serpentine and associated Rocks of the Lizard
District. With Notes on the Chemical Composition of some of
the Rocks of the Lizard District. By W. H. Hudleston. 8vo.
London, 1877.
The Lherzolite of the Ariége. 8vo. London, 1877.
On some Specimens of Gabbro from the Pennine Alps. 8vo.
Truro, 1878.
On the Serpentine and associated Igneous Rocks of the
Ayrshire Coast. 8yo. London, 1878.
204 ADDITIONS TO THE LIBRARY,
Bonney, T. G. Notes on some Ligurian and Tuscan Serpentines.
8vo. London, 1879.
Notes on the Relations of the Igneous Rocks of Arthur’s
Seat. 8vo. London, 1878.
On Professor Dana’s Classification of Rocks. 8vo. London,
1879.
On the Quartz-felsite and associated Rocks at the base of
the Cambrian Series in North-western Caernarvonshire. S8vo.
London, 1879.
The Pre-Cambrian Rocks of Great Britain. S8vo. Bir-
mingham, 1879.
David Thomas Ansted, obituary notice. 8vo. London, 1880.
——. In Memoriam: W. H. Miller. 8vo. Cambridge, 1880.
——. Onsome Serpentines from the Rhetian Alps. 8vo. London,
1880.
Petrological Notes on the Vicinity of the Upper Part of
Loch Maree. 8vo. London, 1880.
——. William Hallowes Miller, obituary notice. 8vo. London,
1880.
——. In Memoriam: W.H. Miller. 8vo. Cambridge, 1881.
. On the Serpentine and associated Rocks of Anglesey. 8vo.
London, 1881.
and F.T.S. Houghton. On some Mica-traps from the Kendal
and Sedbergh Districts. 8vo. London, 1879.
——. On the Metamorphic Series between Twt Hill (Caer-
narvon) and Port Dinorwig. 8vo. London, 1379.
Bosniaski, Sigismondo de. La formazione gessosa e il secondo
piano mediterraneo in Italia. S8vo. Pisa, 1880.
British Museum. Index to the Collection of Minerals, with references
to the Table Cases in which the Species to which they belong are
exhibited. 8vo. London, 1866. Presented by W. Whitaker,
Esq., £.GS.
——. A Guide to the Collection of Minerals. 8vo. London, 1867.
Presented by W. Whitaker, Esq., F.G.S.
Brongniart, A. Recherches sur les graines fossiles silicifiees. Pré-
cédées d’une notice sur ses travaux par J.B. Dumas. 4to. Paris,
1881. Purchased.
Brongniart, C. Notice sur quelques poissons des lignites de Ménat.
8vo. Caen, 1880.
. Rapport sur excursion faite 4 Gisors et aux environs les
16 et 17 mai 1880. 8vo. Rennes, 1880.
et Maxime Cornu. Observations nouvelles sur les épidémies
eévissant sur les insectes. 8vo. Paris, 1830.
ADDITIONS TO THE LIBRARY. 295
Brown, John. A Description of some Borings on the Clifton Estate,
and of the sinking at Clifton Colliery, Nottingham. 8vo. London,
1881.
Brown, Thomas. Illustrations of the Fossil Conchology of Great
Britain and Ireland, with Descriptions and Localities of all the
Species. 4to. London, 1849. Purchased.
Bryce, J. Geology of Clydesdale and Arran. 8vo. London, 1859.
Purchased.
Canada. Geological Survey. Catalogues of the Silurian Fossils of
the Island of Anticosti, by E. Billings. 8vo. Montreal, 1866.
Paleozoic Fossils, vol. 1., 1861-65, by E. Billings.
8vo. Montreal, 1865.
——. -——. Report of Progress for 1878-79. S8yvo. Montreal,
1880.
Capellin, G. Gli strati a Congerie o la formazione Gessoso-solfifera
nella Provincia di Pisa e nei dintorni di Livorno. 4to. Rome,
1880.
Cassell’s Natural History. Edited by P. M. Duncan. Vol. IV.
4to. london, 1880. Presented by Messrs. Cassell, Petter, Galpm,
and Co.
Castro, M. F. de. Discurso leidos ante la Real Academia de
Ciencias Exactas, Fisicas y Naturales en la recepcion publica,
2 de Junio de 1878. 8vo. Madrid, 1878.
On the Influence which a molecular Movement due to
Klectricity may have exerted in certain Geological Phenomena,
namely, the Metamorphism of Rocks and the Formation of
Metalliferous Deposits. 8vo. London, 1880.
Chambers, G. F. A Handbook for Eastbourne &c. 5th edition.
8vo. London, 1873. Presented by W. Whitaker, Esq., F.G.S.
Chaper, Maurice. Note sur le région diamantifére de l Afrique
australe. 8yo. Paris, 1880. Purchased.
Choffat, Paul. Etude stratigraphique et paléontologique des ter-
rains jurassiques du Portugal. Premiére livraison. Le Lias et
le Dogger au Nord du Tage. 4to. Lisbon, 1880.
Church, J. A. The Heat of the Comstock Lode. S8vo. London,
1880.
Clarke, C. B. A Review of the Ferns of Northern India. 4to.
London, 1880.
Cohen, EH. Sammlung von Mikrophotographien zur Veranschau-
lichung der mikroskopischen Structur von Mineralien und Ges-
temen. Lief. 1-4. 4to. Stuttgart, 1881. Purchased.
Collingwood, C. Rambles of a Naturalist on the Shores and Waters
of the China Sea. 8vo. London, 1868. Purchased.
206 ADDITIONS TO THE LIBRARY.
Congrés International de Géologie, tenu 4 Paris, du 29 au 31 aoiit
et du 2 au 4 septembre 1878. Comptes Rendus. 8vo. Paris,
1880. Two copies. Presented by the Foreign Office.
Cope, E. D. On the Extinct Cats of America. 8vo. Salem, 1880.
Catalogue of Vertebrata of the Permian Formation of the
United States. Svo. Salem, 1881.
——. Mammalia of the Lower Eocene Beds. 8vo. Salem, 1881.
On some new Batrachia and Reptilia from the Permian Beds
of Texas; on a Wading Bird from the Amazon Shales; on the
Nimravide and Canidze of the Miocene Period; and on the
Vertebrata of the Wind-River Kocene Beds of Wyoming. 8vo.
Washington, 1881.
—-. Paleontological Bulletin. No. 32. Second Contribution to
the History of the Vertebrata of the Permian Formation of
Texas. Figures. 8vo. Philadelphia, 1881.
The Systematic Arrangement of the Order Perissodactyla,
with a Note on the Structure of the Foot of TYoxodon. S8vo.
Philadelphia, 1881.
Cornu, M., C. Brongniart et Dumas. Sur une épidémie dinsectes
diptcres causée par un Champignon. 8vo. Paris, 1880.
Craven, A. H. Description of three new Species of Land and
Freshwater Shells from Nossi-Bé Island (N.W. coast of Mada-
gascar). Svo. London, 1880.
Monographie du genre Sinusigera, dOrb. 8vo. Brussels,
1880.
Credner, H. Geologischer Fiihrer durch das sichsische Granulit-
gebirge. S8yvo. Leipzig, 1880. Purchased.
Credner, H. Ueber die Vergletscherung Norddeutschlands wahrend
der Kiszeit. S8vo. Berlin, 1880.
Damour, A., und G. vom Rath. Ueber den Kentrolith, eine neue
Mineralspecies. 8vo. Leipzig, 1880.
; . Ueber den Trippkeit, eine neue Mineralspecies. 8vo.
Leipzig, 1880.
Dana, J.D. Appendix (I.) to the 5th edition of Dana’s Mineralogy,
by G. J. Brush, and Appendix II., by E. be Dana. 8vo. New
2 1876. Purchased.
Daubrée, A. Descartes, l’un des créateurs de la cosmologie et de la
géologie. 4to. Paris, 1880.
——, Hxamen minéralogique et chimique de materiaux provenant
de quelques forts vitrifiés de la France. 8vo. Paris, 1881.
Davidson, T. Liste des principaux ouvrages mémoires ou notices
qui traitent directement ou indirectement des Brachiopodes
vivants et fossiles. 1606-1876. 8vo. Brussels, 1880.
ADDITIONS TO THE LIBRARY. 297
Davis, J. W. Report on the Raygill Fissure Exploration Com-
mittee. 8vo. Leeds, 1881.
Dawson, J. W. Sketch of. 8vo. ——, 1875.
Dawson, J. W. Revision of the Land Snails of ‘the Paleozoic Era,
with Descriptions of new Species. 8vo. New Haven, 1880.
Delesse, FE. Sur les études de géologie agronomique aux Etats-Unis
et en particulier sur celles de M. G. H. Cook dans le New-Jersey.
8vo. Paris, 1880.
Delesse, H., et A. De Lapparent. Extraits de Géologie pour les années
1877 et 1878. 8vo. Paris, 1880.
. Revue de Géologie pour les années 1877 et 1878.
Tome XVI. 8vo. Paris, 1880.
Dewalque, G. Prodrome d’une description géologique de la Belgique.
Seconde édition. S8vo. Brussels, 1880.
Sur Vuniformité de la langue Géologique. 8vo. Liége,
1880. :
Doyle, P. Petroleum: its History, Origin, and Use, with reference
to its Advantages and Perils as an Illuminator. 8vo. Brisbane,
1880.
_ Duff, P. A. Ramble among the Fossiliferous Beds of Moray. Fol.
Elgin ?, 1859. Presented by H. B. Woodward, Esq., F.GS.
Duncan, P. M. Scientific Results of the Second Yarkand Mission,
based upon the Collections and Notes of the late Ferdinand
Stoliczka. Syringospheeride. 4to. Calcutta, 1879. Presented by
the India Office.
Duncan, P. M. An Abstract of the Geology of India. Third
edition. Fol. London, 1881.
, and W. Percy Sladen. A Memoir on the Kchinodermata of
the Arctic Sea to the West of Greenland. 4to. London, 1881.
Eichwald, E. De pecorum et pachydermorum reliquiis fossilibus,
in Lithuania, Volhynia et Podolia repertis. 4to. Bonn, 1835,
Purchased.
England and Wales. Geological Survey. Memoirs. Figures and De-
scriptions illustrative of British Organic Remains. Decade XIII.
Ato. London, 1872.
English Channel. Pilote de la Manche. Cote nord de France, par
K. de Courthille avec le concours de F. Hedouin. Tome l. 8vo.
Paris, 1880. Presented by the Dépot de la Marine.
Etheridge, R., jun. A Catalogue of Australian Fossils (including
Tasmania and the Island of Timor), stratigraphically and zoolo-
gically arranged. 8vo. Cambridge, 1878. Purchased.
Evans, John. The Ancient Bronze Implements, Weapons, and Orna
ments of Great Britain and Ireland. 4to. London, 1881.
298 ADDITIONS TO THE LIBRARY.
Evington Coal-Boring Company, Limited. Prospectus. [Containing
Reports by R. Etheridge and James Plant.| Fol. Leicester,
1878? Presented by W. Whitaker, Esq., F.GNS.
Falsan, A., and E. Chantre. Monographie géologique des Anciens
Glaciers et du Terrain Erratique de la partie moyenne du Basin
du Rhone. Text, 2 vols, Svo., 1879-80. Atlas, fol., 1875:
Lyon.
Favre, Ernest. Revue géologique suisse pour Vannée 1880. XI.
8vo. Geneva, 1881.
Festenberg-Packisch, Hermann. Der metallische Bergbau Nieder-
schlesiens unter bentitzung amtlicher Quellen in geognostischer,
historischer und technischer Beziehung. S8vo. Vienna, 1881.
Purchased.
Figari, Antonio. Studii scientifici sull’ Egitto e sue adiacenze com-
presa la penisola dell’ Arabia Petrea. 2 vols. S8vo. Lucca, 1864—
65. Presented by H. Bauerman, Esq., LGN.
Finlands Geologiska Undersokning. Beskrifning till Kartbladet
No. 2, af K. Ad. Moberg. 8vo. Helsingfors, 1880.
Fleming, John. The Lithology of Edinburgh. Edited, with a Me-
moir, by the Rey. John Duns. 8vo. Hdinburgh, 1859. Pur-
chased.
Fontannes, F. Description des Ammonites des calcaires du Chateau
de Crussol, Ardéche. 4to. Lyon, 1879. Purchased.
Foote, Rk. Bruce. On the Geology of parts of the Madras and North
Arcot Districts lying north of the Palar River, and included in
Sheet 78 of the Indian Atlas. S8vo. Calcutta, 1873.
. The Auriferous Rocks of the Dambal Hills, Dharwar Dis-
trict. 8vo. Calcutta, 1874.
The Geological Features of the South Mahratta Country and
the adjacent Districts. Svo. Calcutta, 1876.
Notes on the Representatives of the Upper Gondwana Series
in Trichinopoly and Nellore-Kistna Districts. 8vo. Calcutta,
1878.
. On the Geological Structure of the Eastern Coast from Lati-
tude 15° northward to Masulipatam. 8vo. Calcutta, 1879.
Rough Notes on the Cretaceous Fossils from Trichinopoly
District, collected in 1877-78. 8vo. Calcutta, 1879.
Sketch of the Geology of North Arcot District. 8vo. Cal-
cutta, 1879.
Forrest, Alex. North-west Exploration. Journal of expedition
from De Grey to Port Darwin. 4to. Perth, Western Australia,
1880. Presented by the Governor of Western Australia.
ADDITIONS TO THE LIBRARY. 299
France. Carte géologique detaillée de la France. Mémoires. Miné-
ralogie Micrographique: Roches Eruptives Francaises, par F.
Fouqué et A. M. Lévy. 4to. Paris, 1879. Text and Atlas.
Purchased.
: . ——. Le pays de Bray, par A. de Lapparent. Ato.
Paris, 1879.
Purchased.
—. —. —. Notice explicative. Feuilles 9, 23, 34, 50,
67, 69, 78, 93, 113, 122, 1387, 213 bis, 225 bis, 237. (In slips.)
1881. Purchased.
Fritsch, A. Fauna der Gaskohle und der Kalksteine der Permfor-
mation Bohmens. Band I. Hefte 2 und 3.°4to. Prag, 1880-81.
Gaudry, A. Sur un Reptile trés perfectionné, trouvé dans le terrain
permien. 4to. Paris, 1880.
Sur un nouveau genre de poisson primaire. 4to. Paris,
1881.
Geikie, A. Outlines of Field Geology. 8vo. London, 1876. Pre-
sented by W. Whitaker, Hsq., F.GS.
Geikie, J. Prehistoric Europe: a geological sketch. Svo. London,
1881. Purchased.
Gemitz, H. B. Nachtrige zur Dyas. I. Mit Beitragen der Herren
Drude, Vetter und Weiss. 4to. Cassel, 1880.
Geyler, H. T. Phytopaleontologie. 8vo. ——-,1878. Presented
by W. Whitaker, Esq., F.GS.
Giebel, C.G. Die Saugethiere in Zoologischer, anatomischer und
paliontologischer Beziehung. 2nd edition. 8vo. Leipzig, 1859.
Purchased.
Gilpin, H. The Mines and Mineral Lands of Nova Scotia. 8vo.
Halifax, N.S., 1880.
Goodyear, W. A. Harthquake and Volcanic Phenomena, December
1379 and January 1880, in the Republic of Salvador, Central Ame-
rica. Svo. Panama, 1880. (Iwo copies.)
Gosse, Philip Henry. Omphalos: an attempt to untie the geological
knot. 8vo. London, 1857. Purchased.
Gosselet, J. Constitution géologique du Cambresis. Svo. Cambrai?
1865. Presented by W. Whitaker, Esq., F.GN.
Esquisse géologique du département du Nord et des contrées
voisines. Fasc. 1 et 2. 8vo. Lille, 1873-76. Presented by W.
Whataker, Esq., 2.GS.
Gosselet, J. Le terrain dévonien des environs de Stolberg. 8vo,
Lille, 1876.
——. Relations des sables d’Anvers avec les systemes Diestien et
Boldérien. S8vo. Lille, 1876.
"aco ADDITIONS TO THE LIBRARY.
Gosselet, J. Compte-rendu de lVexcursion dans les Ardennes du 23
aout au 5 septembre 1876. 8vo. Lille, 1877.
Quelques réflexions sur la structure et lage du terrain
houiller du Nord de la France 4 Voccasion du Mémoire de M.
Breton et de celui de M. ’Abbé Boulay. 8vo. Lille, 1877.
——. Sur quelques fossiles trouvés dans le silurien des Ardennes.
8vo. Lille, 1877.
Apercu sur la constitution géologique de la Forét de Mormal.
8vo. Lille, 1878.
Excursion dans les tranchées du chemin de fer de Cambrai
au Quesnoy. 8vo. Lille, 1878.
——. le marne de la Porquerie (€océne inférieur). 8vo. Lille,
1878.
——. Le calcaire dévonien supérieur dans le N.-E. de larrondisse-
ment d’Avesnes et documents pour l’étude des schistes de Famenne.
8yvo. Lille, 1878.
——. Documents nouveaux pour l’étude du Famennien. Tran-
chées du chemin de fer entre Féron et Semeries. Schistes de Sains.
8vo. Lille, 1879.
Le calcaire de Givet. 3™° et 4™° parties, suivies de consi-
dérations sur la terminaison orientale de la grand faille. 8vo.
Lille, 1879.
——. IT /argile a silex de Vervins. 8vo. Liaille, 1879.
——. Laroche aTfépin. Contact du terrain silurien et du terrain
dévonien sur les bords de la Meuse. 8vo. Lille, 1879.
Notice necrologique sur Jean-Baptiste-Julien d’Omalius
d’Halloy. 8vo. Lille, 1879.
——. De Vusage du droit de priorité et de son application aux
noms de quelques Spiriferes. 8vo. Lille, 1880.
——. Les roches cristallines des Ardennes. 8vo. Lille, 1880.
——. Notes sur les sables tertiaires du Plateau del’Ardenne. Lille,
1881.
——. Terrain diluvien de la Vallée de la Somme. 8vo. Lille,
1880.
——. Troisiéme note sur le Famennien. Tranchée du chemin de
fer du Luxembourg. Les schistes de Barvaux. 8vo. Lille, 1880.
Esquisse géologique du Nord de la Frauce et des contrées
voisines. 1% fascicule. Terrains primaires. Text and Plates. 8vo.
Lille, 1880.
—— et Henri Rigaux. Mouvement du sol de la Flandre depuis les
temps géologiques. 8yvo. Lille, 1878.
Gotthard Tunnel. Geologische Tabellen und Durchschnitte uber den
Grossen Gotthardtunnel. Lief.4—-6. 4to. Zurich, 1877-79. Pur
chased.
ADDITIONS TO THE LIBRARY. 301
Gregorio, Antono de. Fauna di 8. Giovanni [larione (Parisiano).
Parte 1°. Cefalopodi e Gasteropodi. Fasc. 1. 4to. Palermo,
1880. |
Giimbel, C.W. Geognostische Mittheilungen aus den Alpen. VII.
8vo. Munich, 1880.
Nachtrage zu den Mittheilungen iiber die Wassersteine
(Enhydros) von Uruguay und ber einige stid- und mittel-ameri-
kanische sogenannten Andesite. 8vo. Munich, 1881.
Ginther, A.C. L.G. An Introduction to the Study of Fishes. 8vo.
Edinburgh, 1880. Purchased.
Gutch’s Literary and Scientific Register and Almanack for the year
1867. (Geology, by J. B. Jukes.) 12mo. London, 1866. Presented
by W. Whitaker, Esq., F.G.S.
Habenicht, H. Die Grundzige im geologischen Bau Europa’s, mit
einer Karte, “‘ Die Verbreitung der Kruptiv- und Uebergangs-
gesteine in Europa,” und funf Nebenkarten. 8vo. Gotha, 1881,
.Hahn, Otto. Die Meteorite (Chondrite) und ihre Organismen. 4to.
Tubingen, 1880. Purchased.
Haniel, John. Die Flotzlagerung in der Stoppenberger und Horst-
Hertener Mulde des Westfilischen Steinkohlengebirges. to.
Essen, 1881. Purchased.
Hann, J., F. vy. Hochstetter und A. Pokorny. Allgemeine Erdkunde.
Ein Leitfaden der astronomischen Geographie, Meteorologie, Geo-
logie und Biologie. 8ve. Prague, 1872. Purchased.
Hawes, G.W. The Albany Granite, New Hampshire, and its con-
tact phenomena. S8vo. New Haven, 1881.
Hébert, E. Histoire géologique du canal de la Manche. 4to. Paris,
1880.
Recherches sur la craie superieure du versant septentrional
des Pyrénées. 4to. Paris, 1880.
Nomenclature et classification géologiques. 8vo. Paris,
1881.
Heer, O. Flora fossilis Artica. Band 2. 4to. Winterthur, 1871.
Purchased.
Band 6. 1 Abth. 4to. Zurich, 1880. Purchased.
Hicks, Henry. On some recent researches among Pre-Cambrian
Rocks in the British Isles. 8vo. London, 1881.
Hill, E., and 7. G. Bonney. The Precarboniferous Rocks of Charn
wood Forest. Part 1. S8vo. London, 1877.
Part 2. 8vo. London, 1878.
——. Part3. 8vo. London, 1880.
Hinde, G. J. Fossil Sponge-spicules from the Upper Chalk, found
in the interior of a single flint-stone from Horstead in Norfolk.
8vo. Munich, 1880.
302 ADDITIONS TO THE LIBRARY.
Hitchcock, E. The Religion of Geology. 8vo. London, 1851.
Purchased.
Hornes, R. Die Trilobiten-Gattungen Phacops und Dalmanites
und ihr vermuthlicher genetischer Zusammenhang. 8vo. Vienna,
1830.
——. Materialien zu einer Monographie der Gattung Megalodus
mit besonderer beriicksichtigung der mesozoischen Formen. 4to.
Vienna, 1880.
und M. Auinger. Die Gasteropoden der Meeres-ablagerungen
der ersten und zweiten miocinen Mediterran-stufe in der oster-
reichisch-ungarischen Monarchie. Parts 1&2. 4to. Vienna,
1879-80.
Holm, G. Anteckningar om Wahlenbergs Illcenus crassicauda. 8vo.
Stockholm, 1880.
Bemerkungen iiber IJlenus crassicauda. 8vo. Berlin, 1880.
Hudleston, W. H. Contributions to the Paleontology of the York-
shire Oolites. S8vo. London, 1881. :
Hull, E. On the Geological Structure of the Northern Highlands of
Scotland ; being notes of a recent tour. 8vo. Dublin, 188].
The Coalfields of Great Brirain; their History, Structure,
and Resources. Fourth edition. 8vo. London, 1881.
Idria. K.-k. Bergdirection. Das k.-k. Quecksilberwerk zu Idria in
Krain. 4to. Vienna, 1881. Presented by the K.-k. Ackerbaumt-
nisterium, Vienna.
Tllinois. Geological Survey. Report. Vol. 3, by A. H. Worthen,
H. Engelmann, H.C. Freeman, H. M. Bannister, and F. B. Meek.
Ato. Springfield, Ill., 1868. Presented by the late Dr. J. J. Bigsby,
JBL TiS, JEG IS
. —. Vol. 4, by A. H. Worthen, H. M. Bannister,
ae H. Bradley, H. A. Green, J. 8. Newberry, and Leo Lesquereux.
Ato. Springfield, Ill.,1870. Presented by the late Dr. J. J. Bigsby,
JBI gShy, HAAG HS
——. : . Vol. 5, by A. H. Worthen, J. Shaw, and F.
B. Meek. 4to. Springfield, Ill., 1873. Presented by the late
Dr. J. J. Bigsby, LLS., F.GS.
as, ——. Vol. 6, by A. H. Worthen, G. C. Broadhead,
KE. T. Cox, 0. St. J ohn, and F. B. Meek. to. Springfield, IIL,
1875. Presented by the late Dr. J. J. Bigsby, P_BS., EGS.
India. Geological Survey. Memoirs. Vol. xv. Part 2. 1880.
Vol. xvi. Part 1. 1880.
. Paleontologia Indica. Ser.10. Indian Tertiary and
Post-tertiary Vertebrata. Vol. i. Part 4. Supplement to Crania
of Ruminants, by R. Lydekker. 1880.
Ser. 10. Vol.i. Part 5. Siwalik and Narbada
Proboscidia, by R. Lydekker. 1880.
ADDITIONS TO THE LIBRARY. 303
India. Geological Survey. Paleontologia Indica. Ser. 13.
Salt-Range Fossils, by W.Waagen. Part2. 1880.
ee. Records, Vol) xi. /Parts 3&4. 1880,
Molt xaiveinanismivanece Toole
Indiana. Department of Statistics and Geology of the State of In-
diana. First Annual Report, 1879. 8vo. Indianopolis, 1880.
Jack, R. L. Report on the Geology and Mineral Resources of the
District between Charters Towers Goldfield and the Coast. 4to.
Brisbane, 1879.
Report to the Honourable the Minister for Mines on the
Bowen River Coalfield. 4to. Brisbane, 1879.
Jeffreys, J. Gwyn. The French Deep-sea Exploration in the Bay
of Biscay. 8vo. London, 1880.
—. Deep-sea Exploration. 8vo. London, 1881.
Jervis, G. Dell’ Oro in Natura. 8vo. Turin, 1880.
Jones, T. Rupert. Unio and Paludine from the Wealden Beds of
Kent, in the collection of Mr. W. Harris of Charing. 8vo. London,
1860.
Note on the Well lately sunk at Wokingham, Berkshire.
8yo. London, 1880.
Report of the Excursion of the Geologists’ Association to
Camberley, April 24, 1880. 8vo.. London, 1880.
Fossil Foraminifera of the Carboniferous Limestone. (Review
of Memoirs by V. von Moller.) Slip. London, 1881.
On the Geology and Physical Features of the Bagshot Dis-
trict. 8vo. London, 1881.
Julien, A. A. On Biotite as a Pseudomorph after Olivine. 8vo.
New York, 1878.
——. On the Geological Action of the Humus Acids. 8vo. Salem,
1880.
Karsten, G. Beitrige zur Landeskunde der Herzogthumer Schleswig
und Holstein Reihe2. Heftelund2. 4to. Berlin, 1869 & 1872.
Purchased.
Kobell, V. Obituary notices of Johann von Lamont, Carl Friedrich
Mohr, Heinrich Wilhelm Dove, Aug. Heinrich Rudolph Grisebach,
Bernhard v. Cotta, and J. F. Brandt. 8vo. Munich, 1880.
——-. Ueber Polarisationsbilder an Zwillingen zweiaxiger Kry-
stalle. S8vo. Munich, 1880.
Kuntze, O. Ueber Geysirs und nebenan entstehende verkieselte
Baume. 4to. Stuttgart, 1880.
Leidy, J. Bathygnathus borealis, an extinct Saurian of the New
Red Sandstone of Prince Edward’s Island. 4to. Philadelphia,
18381.
304 ADDITIONS TO THE LIBRARY.
Leidy, J. Remarks on Bathygnathus borealis. 4to. Philadelphia,
1881.
Locard, A. Nouvelles recherches sur les argiles lacustres des ter-
rains quaternaires des environs de Lyon. 8vo. Lyon, 1880.
Purchased.
Loretz, H. Ueber Schieferung. 8vo. Frankfurt a. M., 1880.
Macpherson, J. Uniclinal Structure of the Iberian Peninsula. S8vo.
Madrid, 1880.
Maestre, Amaleo. Descripcion geologica industrial de la cuenca car-
bonifera de San Juan de las Abadesas en la Provincia de Gerona.
Ato. Madrid, 1855. Purchased.
Mallet, F. R. On the Ferruginous Beds associated with the Basaltic
Rocks of North-eastern Ulster, in relation to Indian Laterite.
8vo. Calcutta, 1881.
Marcou, Jules. Sur les colonies dans les roches taconiques des bords
du lac Champlain. 8vo. Paris, 1881.
Marsh, O. C. Notice of Jurassic Mammals representing two new
Orders. S8vo. New Haven, 1880.
—. The Sternum in Dinosaurian Reptiles. 8vo. New Haven,
1880.
A new Order of extinct Jurassic Reptiles (Ceeluria). 8vo.
New Haven, 1881.
Discovery of a fossil Bird in the Jurassic of Wyoming. 8vo.
New Haven, 1881.
——. Note on American Pterodactyls. &vo. New Haven, 1881.
——., Principal Characters of American Jurassic Dinosaurs. Part
IV. Spiral Cord, Pelvis, and Limbs of Stegosaurus. 8vo. New
Haven, 1881.
Martin, K. Die Tertiirschichten auf Java. 4to. Leiden, 1880.
Purchased.
Mathews, W. The Flora of Algeria, considered in relation to the
Physical History of the Mediterranean Region and supposed Sub-
mergence of the Sahara. 8vo. London, 1880.
Mawe, John. Travels in the Gold and Diamond Districts of Brazil.
Svo. London, 1825. Purchased.
Meli, Romolo. Sui dintorni di Civitavecchia. 4to. Rome, 1879.
Meneghini, G. Fossili oolitici di Monte Pastello nella provincia di
Verona. 8vo. Pisa, 1880.
——. Nuovi fossili siluriani di Sardegna. 4to. Rome, 1880.
Merccy, N. de. Sur un sondage exécuté a Saint-Blimont (Somme).
Svo. Amiens, 1879.
- ADDITIONS TO THE LIBRARY. 395
Mercey, N. de. . Composition des sables de Bracheux et mode d’origine
de l’argile plastique, premier produit d’une émanation terminée par
le dépot du caleaire de Mortemer, d’aprés des coupes du chemin
de fer de Compicgne (Oise) & Roye (Somme). 8vo. Paris, 1880.
Compte-rendu du course de la Soci¢té géologique de France
& Maignelay le samedi 7 septembre 1878. S8vo. Paris, 1880.
Note sur la confusion résultant de ’emploi de la dénomina-
tion @argile a silex appliquée 4 deux dépots placés, Pun a la base,
- et l'autre au sommet de la série tertiaire du Nord de la France. 8vo.
Lille, 1880.
Observations a loccasion de quelque travaux publiés dan
les Annales de la Société géologique du Nord sur le quaternaire
ancien. 8vo. Lille, 1880.
Remarques sur la classification du terrain crétacé supérieur.
8vo. Paris, 1880.
—. Sur les couches de Sinceny. 8vo. Paris, 1880.
Minnesota. Geological and Natural-History Survey. Sixth Annual
Report, for the year 1877. 8vo. Minneapolis, 1878. Presented
by Prof. N. H. Winchell, State Geologist.
Seventh Annual Report, for the Ne 1878. 8vo.
Minneapolis, 1879. Presented by Prof. N. H. Winchell, State
Geologist.
=——,
Eighth Annual Report, for the year 1879. 8vo.
Saint Paul, 1880. Presented by the State Geologist.
Moyjsisovics, HL. v., H. Tietze, und A. Bittner. Grundlinien der Geo-
logie von Bosnien-Hercegovina. S8vo. Vienna, 1880.
Ueber heteropische Verhiltnisse 1m Triasgebiete der lom-
_bardischen Alpen. S8vo. Vienna, 1880.
Morris, John. Coal; its Geological and Geographical Position. 8vo.
London, 1862. Presented by Prof. T. Rupert Jones, P.RS.,
areeGsS.
Morton, G. H. The Carboniferous Limestone and Cefn-y-fedw Sand-
stone of the Country between Llanymynech and Minera, North
Wales. 8vo. London, 1879. Purchased.
Mourlon, Michel. Géologie de la Belgique. 2 vols. 8vo. Brussels,
1880 & 1881.
ey. | Purchased.
Murray, Alex. Report on the Gold Region near Brigus, Conception
Bay, Newfoundland. Fol. St. John’s, 1880.
Nathorst, A. G. Berattelse, afgifven till Kongl. Vetenskaps-Akade-
mien, om en med understod af allminna medel utford vetenskaplig
resa till England. 8vo. Stockholm, 1880. Presented by (. Reid,
Esq., F.GS.
VOL. XXXVII. ze
306 ADDITIONS TO THE LIBRARY.
Naumann, C. F. Lehrbuch der Geognosie. Paliontologischer Atlas.
70 Tafeln. 4to. Leipzig,n.d. Purchased.
New Jersey. Geological Survey. Annual Report for the year 1880.
8vo. Trenton, N.J., 1880. (G. H. Cook, State Geologist.)
New South Wales. Department of Mines. Annual Report for 1878.
Ato. Sydney, 1879.
for 1879, and Maps. 4to. Sydney, 1880.
Report upon certain Museums for Technology, Science, and
Art, also upon Scientific, Professional, and Technical Instruction
and Systems of Evening Classes in Great Britain and on the Con-
tinent of Europe. By A. Liversidge. Fol. Sydney, 1880.
New York, Natural History of. Paleontology. Vol. V. Part 2
(Text and Plates). By James Hall. 4to. Albany, 1879.
New Zealand. Colonial Museum and Geological Survey Department.
Manual of the New-Zealand Mollusca. By F.W. Hutton. 8vo.
Wellington, 1880.
Palaontology of New Zealand. Part IV. Corals and
Bry ozoa of the Neozoic Period in New Zealand. By J. KE. Tenison
Woods. 8vo. Wellington, 1880.
. Colonial Musewm. Meteorological Report, 1880: including
returns for 1877, 1878, 1879, and averages for previous years.
8vo. Wellington, 1882.
——. -——. 15th Annual Report. 8vo. Wellington, 1880.
New-Zealand Court, International Exhibition, Sydney, 1879. Ap-
pendix to Official Catalogue. 8vo. Wellington, 1880. Pre-
sented by the Colonial Government.
Nicholson, H. A. On the Structure and Affinities of the Genus
Monticulipora and its Subgenera, with critical Descriptions of
illustrative Species. 8vo. Hdinburgh, 1381.
** Norwegian North-Atlantic Expedition.” Den Norske Nordhavs-
Expedition, 1876-1878. Chemi af H. Tornée. 4to. Christiania,
1880. Presented by the Meteorological Institute, Christiania.
——. =. Zoology. Fiske, af R. Collett. 4t0. Christiama,
1880. Presented by the Meteorological Institute, Christiania.
Ombon, G. Denti di Ippopotamo da aggiungersi alla fauna fossile
del Veneto. 4to. Venice, 1880.
Ormathwaite, John Lord. Astronomy and Geology compared. 8vo.
London, 1872. Purchased.
Paléontologie francaise. 1" Série. Animaux invertébrés. Terrain
Jurassiqué. Tome III. Livr.3 et 9. Gastéropodes. 8vo. Paris?
Purchased.
——, —, ——. Livr. 44-46. Echinodermes nesuliens
par G.Cotteau. 8yvo. Paris, 1880-81. Purchased.
ADDITIONS TO THE LIBRARY. 307
Parker, J. Map and Sections of Strata south of Oxford, prepared
for the meeting of the Excursion of the Geological Association
May 17, 1880. 8vo. Oxford, 1880. Presented by W. Whitaker,
Esq., F.GS.
Pengelly, W. Notes on Boulders and Scratched Stones in South
Devon. Part 3. 8vo. Plymouth, 1880.
Notes on recent Notices of the Geology and Paleontology of
Devonshire. Part 7. 8vo. Plymouth, 1880.
Sixteenth and concluding Report of the Committee, consist-
ing of John Evans, Sir John Lubbock, Bart., Edward Vivian, G.
Busk, W. Boyd Dawkins, W. A. Sanford, J. E. Lee, and W. Pen-
gelly, appointed for the purpose of exploring Kent’s Cavern, De-
vonshire. 8vo. London, 1880.
Percy, C. M. Winding and Overwinding. 8vo. Wigan, 1880.
Pettersen, Karl. Lofoten og Vesteraalen. 8vo. Christiania, 1881.
Piret, F. M. La fontaine ardente de Saint-Barthélemy (Isére). Gas
naturel, Charbon, Pétrole. 8vo. Grenoble, 1881.
Ponzi, G. I terremoti delle epoche subappennine. 8vo. Rome,
1880.
Sui lavori del Tevere, e sulle variate condizioni del suolo
romano. 4to. Rome, 1880.
Preussen und die thiiringische Staaten. Geologische Specialkarte.
Erliuterungen. Gradabtheilung 67. Nos. 53, 54, 59, 60. 8vo.
Berlin, 1880. Presented by the Prussian Minster of Manu-
fauctures, Trade, and Aris.
Gradabtheilung 68. Nos. 49 & 55. 8vo.
Tediine 1880. Presented by the Prussian Minister of Manufactures
fc.
—_——— ed
e
Gradabtheilung 80. Nos. 19, 20, 25, 26,
31,32. 8vo. Berlin, 1880. Presented by the Prussian Minister
of Manufactures &c.
Quenstedt, F.A. Petrefactenkunde Deutschlands. Abth.1. Band VI.
Heft 5 (Korallen). Text, 8vo; Atlas, 4to. Leipzig, 1880. Pur-
chased,
. Abth. 1. Band VI. Heft 6 (Korallen, Heft 11).
Text, 8vo; Atlas, fol. Leipzig, 1880. Purchased.
Reade, T. M. A Problem for Irish Geologists in Postglacial Geology.
8vo. Dublin, 1879.
—. Oceans and Continents. 8vo. London, 1880.
——. The Glacial Beds of the Clyde and Forth. 8vo. Liverpool,
1880.
Reinsch, Paulus Friedrich. Neue Untersuchungen iiber die Mikro-
308 ADDITIONS TO THE LIBRARY. '
sstruktur der Steinkohle des Carbon, der Dyas und Trias. 4to.
Leipzig, 1881. Purchased.
Renault, B. Cours de botanique fossile fait au Muséum d’Histoire
naturelle. Premiere Année. 8vo. Paris, 1881. Purchased.
Renevier, H. Orographie de la partie des Hautes-Alpes calcaires
comprise entre le Rhone et le Rawyl (groupes des Diablerets et
du Wildhorn). 8vo. Lausanne, 1880.
——. Rapport sur la marche du Musée géologique vaudois en
1879. 8vo. Lausanne, 1880.
Seconde compte-rendu de la Commission géologique interna-
tionale pour l unification des procédés graphiques. 8vo. Lausanne,
1881.
Reyer, H. Allgemeine Geschichte des Zinnes. 8vo. Vienna, 1880.
——. Die Bewegung im Festen. 4to. Stuttgart, 1880.
-——. Zinn: Eine geologisch-montanistisch-historische Mono-
grafie. 8vo. Berlin, 1881.
Ricketts, C. On the Carboniferous Limestone near Skipton and in
North Derbyshire. 8vo. Liverpool, 1880.
Riviére, Emile. Paléoethnologie. De lantiquité de ’homme dans
les Alpes-Maritimes. Livr. 7. 4to. Paris, 1879. Purchased.
——, = Livr. 8. -4to! Paris) 1Seilieercnoscoe
Ruskin, J. Deucalion. Collected Studies of the Lapse of Waves
and Life of Stones. Part VII. 8vo. Sunnyside, Orpington, 1880.
Rutot, A., et H. van den Broeck. Les phénoménes post-tertiaires en
Belgique dans leurs rapports avec lorigine des dépéts quaternaires
et modernes. 8vo. Lille, 1880.
Sandberger, F. Kin Beitrag zur Kenntniss der unterpleistocinen
Schichten Englands. 4to. Cassel, 1880.
. Ueber die Bildung yon Erzgiingen mittelst Auslaugung des
Nebengesteins. Svo. Berlin, 1880.
Saporta, G. de, et A. F. Marion. L’évolution du régne vegetal.
Les Cryptogames. 8vo. Paris, 1881.
Sartorius von Waltershausen, W .Der Aetna. Herausgegeben, selbst-
stindig bearbeitet und vollendet von A. von Lasaulx. Band I. &
II. 4to. Leipzig, 1880. Purchased.
Sauvage, H. E. Recherches sur les poissons fossiles du terrain
erétacé de la Sarthe. S8vo. Paris, 1872.
——. Notes sur les reptiles fossiles. Svo. Paris, 1873.
-——. Notice sur les poissons tertiaires de VAuvergne. §8vyo.
Toulouse, 1874.
Notes sur les reptiles fossiles. 8vo. Paris, 1876,
ADDITIONS TO THE LIBRARY. : 309
Sauvage, H. H.. Sur les Lepidotus palliatus et Spherodus gugas.
8vo. Paris, 1877.
Etude sur les poissons et les reptiles des terrains crétacé
et jurassique supérieur de l’Yonne. 8yo. Auxerre, 1880 (?).
Etude sur les poissons des faluns de Bretagne. 4to. Chalon-
sur-Sadne, 1880.
Saxony. Geologische Landesuntersuchung des Kongreichs Sachsen.
Erlauterungen zur geologischen Specialkarte. Blatt 28,75, & 115.
8vo. Leipzig, 1880.
Schmid, E. E. Die quarzfreien Porphyre des centralen Thiringer
Waldgebirges und ihre Begleiter. 4to. Jena,1880. Purchased.
Schmidt, A. Die Zinkerz-Lagerstatten von Wiesloch (Baden). 8vo.
Heidelberg, 1881.
Schmidt, Oscar. Die Spongien des Meerbusen von Mexico (und des
earaibischen Meeres). Heft 2. 4to. Jena, 1880. Purchased.
Schédler, F. The Treasury of Science, Natural and Physical.
Translated by H. Medlock. 8vo. London, 1862. Presented by
W. H. Dalton, Esq., F.GS.
Scrope, G. Poulett. On the supposed Influx of Water to the Interior
of the Globe as the Cause of Volcanic Action. 8vo. London, 1869.
Presented by Prof. J. W. Judd, F.RS., Sec. GS,
On the Character and Composition of Lavas. 8vo. London,
1870. Presented by Prof. J. W. Judd, F.RS., Sec. GS.
——. Notes on the late Eruption of Vesuvius. 8vo. London,
1872. Presented by Prof. J. W. Judd, F.RS., Sec. GS.
. On “ Blocky” Rock-surfaces, and the Theory of the Shrink-
ing Nucleus of the Globe. 8vo. London, 1873. Presented by Prof.
HaWeadudd, Fis.
Scudder, S. H. The Devonian Insects of New Brunswick. en.
Boston, 1880.
. The Structure and Affinities of Hwphoberia, Meek & Worthen,
a Genus of Carboniferous Myriapoda. 8vo. New Haven, 1881.
Sheafer, P. W. The Anthracite Coalfields of Pennsylvania, and their
Exhaustion. 8vo. Haston, 1880 (?).
Simpson-Baikie, H. The International Dictionary for Naturalists
and Sportsmen, in English, French, and German. 8vo. London,
~ 1880.
Sollas, W. J. On the Ventriculite of the Cambridge Upper Green-
sand. S8vo. London, 1873.
——. On Evolution in Geology. 8vo. London, 1877.
——. On Pharetrospongia Strahani, Sollas, a fossil Holorhaphidote
Sponge from the Cambridge ‘‘ Coprolite”-bed. 8vo. London,
1877.
310 ADDITIONS TO THE LIBRARY.
Sollas, W. J... On Stauronema, a new Genus of fossil Hexactinellid
Sponges, with a Description of its two Species, S. Carteri and
S. lobata. 8vo. London, 1877.
On the Changes produced in the Siliceous Skeletons of cer-
tain Sponges by the Action of Caustic Potash. 8vo. London,
1877.
On the Perforate Character of the Genus Webbina, with a
Notice of two new Species, W. levis and W. tuberculata, from the
Cambridge Greensand. 8vo. London, 1877.
On the Structure and Affinities of the Genus Stphonia. 8vo.
London, 1877.
. On the Structure and Affinities of the Genus Catagma. 8vo.
London, 1878.
On two new and remarkable Species of Cliona. 8vo. London,
1878,
Observations on Dactylocalyx pumiceus (Stutchbury), with
a Description of a new Variety, Dactylocalyx Stutchburyi. 8vo.
London, 1879.
On Plectronella papillosa, a new Genus and Species of Echi-
nonematous Sponge. 8vo. London, 1879.
On Plocamia plena, a new Species of Echinonematous Sponge.
8vo. London, 1879.
——. On some Three-toed Footprints from the Triassic Conglo-
merate of South Wales. 8vo. London, 1879.
——. On the Silurian District of Rhymney and Pen-y-lan, Cardiff.
8vo. London, 1879.
——. On some Eskimos’ Bone-Implements from the East Coast
of Greenland. 8vo. London, 1880.
. On the Flint Nodules of the Trimmingham Chalk. 8vo.
London, 1880.
——, On the Structure and Affinities of the Genus Protospongia
(Salter). 8vo. London, 1880.
——. The Sponge-fauna of Norway: a Report on the Rev. A. M-
Norman’s Collection of Sponges from the Norwegian Coast. 8vo.
London, 1880.
Sollas, W. J., and A. J. Jukes-Brown. On the included Rock-frag-
ments of the Cambridge Upper Greensand. 8yvo. London, 1873
South Australia. Public Works Report. Report from the Public.
Works Department for the Half Year ended 30th June, 1878. 4to.
Adelaide, 1879. Presented by the Colonial Government.
Spain. Comision del mapa geologico de Espana. Boletin. Tomo VII-
Cuadernol1 &2. 8vo. Madrid, 1880.
Spencer, J. W. Discovery of the Preglacial Outlet of the Basin of
ADDITIONS TO THE LIBRARY. 3I1
Lake Erie into that of Lake Ontario; with Notes on the Origin
of our Lower Great Lakes. 8vo. Philadelphia, 1881.
Spencer’s Illustrated Leicester Almanack dc. for 1880. 8vo.
Leicester, 1880. Presented by W. Whitaker, Esq., F.G.S.
Spratt, T. A. B. Report on the Present State of the Navigation of
the River Mersey (1880). 8vo. London, 1881.
Struckmann, C. Die Wealden-Bildungen der Umgegend von Han-
nover. 8yvo. Hannover, 1880. (Two copies.)
Ueber den Parallelismus der hannoverschen und der
euglischen oberen Jurabildungen. 8vo. Stuttgart, 1881.
Swansea. British Association. The Official Guide and Handbook
to Swansea and District, by 8. C. Gamwell. 8vo. Swansea, 1880.
Presented by W. Whitaker, Esq., F.GS.
Switzerland. Comnussion géologique suisse. Materiali per la carta
geologica. Vol. XVII. Il canton Ticino meridionale ed 1 paesi
finitimi, per Torquato Taramelli. Appendice ed Indice. 4to.
Bern, 1880.
: Beitrige zur geologischen Karte. Lieferung 20. Der
mechanische Contact von Gneiss und Kalk im Berner Oberland
von A. Baltzer. 4to. Bern, 1880.
Tate, R. The Anniversary Address of the President to the Adelaide
Philosophical Society. S8vo. Adelaide, 1879.
——. The Natural History of the Country around the Head of the
Great Australian Bight. 8vo. Adelaide, 1879.
——. Zoologica et Paleontologica Miscellanea, chiefly relating to
South Australia. 8vo. Adelaide, 1879.
Taylor, J. E. A Guide to the Ipswich Museum. 8vo. Ipswich,
1871. Presented by W. Whitaker, Esq., F.GS.
Terquem, O. Essai sur le classement des animaux qui vivent sur
la plage et dans les environs de Dunkerque. 8vo. ——, 1880 (?).
Thomson, James. Contributions to our Knowledge of the Rugose
Corals from the Carboniferous Limestone of Scotland. 8vo. Glas-
gow, 1880.
Thureau, G. Synopsis of a report on Mining in California and
Nevada, U.S. A. 8vo. Melbourne, 1879.
Trafford, F. W. C. Souvenir de ’amphiorama, ou la vue du monde ~
pendant son passage dans une comete. 8vo. Zurich, 1880.
=== Homnelny Weel.
Tribolet, Maurice de. Sur le gault de Renan. 8vo. Delémont,
1877. Presented by A. J. Jukes-Browne, Hsq., F.G.S.
Tullberg, S.A. Om Agnostus-arterna i de kambriska aflagringarne
‘vid Andrarum. 4to. Stockholm, 1880.
312 ADDITIONS TO THE LIBRARY.
Tullbery, S.A. Om lagerfoljden ide kambriska och siluriska aflag-
ringarne vid Rostanga. 8vo. Stockholm, 1880.
——. Tvenne nya graptolitsligten. Svo. Stockholm, 1880.
Ueber Versteinerungen aus den Aucellen-Schichten Novaja-
Semljas. 8vo. Stockholm, 1881.
Twelvetrees, W. H. Ona Labyrinthodont Skull (Platyops Rickardt,
Twelvetr.) from the Upper Permian Cupriferous Strata of Karga-
linsk near Orenburg. 8vo. Moscow, 1880.
On Theriodont Humeri from the Upper Permian Copper-
bearing Sandstones of Kargalinsk near Orenburg. 8vo. Moscow,
1880.
United States. Geographical and Geological Survey of the Rocky-
Mountain Region. (J. W. Powell, in charge.) Report on the Geo-
logy of the High Plateaus of Utah, by C. E. Dutton. 4to; Atlas
fol. Washington, 1880.
Geological and Geographical Survey of the Territories. Bul-
let Voli Voy Nowa ess:
——. ——. ——. Vol. VI. No.1. 1881.
. Miscellaneous Publications. No. 12. History of North
American Pinnipeds: a Monograph of the Walruses, Sea-lions,
Sea-bears, and Seals of North America, by Joel Asaph Allen. 8yo.
Washington, 1880.
. Report. Vol. XII. Fresh-water Rhizopods of North
America, by Joseph Leidy. 4to. Washington, 1879.
Ussher, W. A. E. On the Geology of Parts of Devon and West
Somerset north of South Molton and Dulverton. 8vo. Taunton,
1881.
Van den Broeck, EK. Du role de Vinfiltration des eaux météoriques
dans l’altération des dépéts superficiels. 8vo. Paris, 1880.
——. Mémoire sur les phénomeénes d’altération des dépdts super-
ficiels par Vinfiltration des eaux météoriques étudiés dans leurs
rapports avec la géologie stratigraphique. 4to. Brussels, 1881.
Observations nouvelles sur les sables diestiens et sur les
dépots du Bolderberg. 8vo. Brussels, 1881.
Van den Broeck, E., et H. Miller. Wes Foraminiféres des couches
pliocenes de la Belgique. 1" Partie. Hsquisse géologique et palé-
ontologique des dépdts pliocénes des environs d’Anvers, par E.
van den Broeck. Fascicule 2. Les sables moyens et les sables
supérieurs d’Anvers. 8yo. Brussels, 1878.
Vetter, B. Die Fische aus dem lthographischen Schiefer in Dres-
dener Museum. 4to. Cassel, 1881.
Victoria. Mineral Statistics of Victoria for the year 1879. 4to.
Melbourne, 1880. Presented by the Minister of Mines.
ADDITIONS TO THE LIBRARY. 313
Victoria. Geological Survey. Report of Progress, No. VI. 8vo.
Melbourne, 1880. Presented by the Minister of Mines.
Report of the Chief Inspector of Mines to the Honourable the
Mimster of Mines for the year 1879. 4to. Melbourne, 1880.
Reports of the Mining Surveyors and Registrars. Quarter
ended 31st March, 18380. 4to. Melbourne, 1880. Presented by
the Minister of Mines.
Quarter ended 30th June, 1880. Fol. Melbourne,
1880. Presented by the Minster of Mines.
Quarter ended 30th September, 1880. 4to. Mel-
bourne, 1880. Presented by the Minister of Mines.
. Quarter ended 3lst December, 1880. 4to. Mel-
bourne, 1880. Presented by theMimster of Mines.
Vogdes, A. W. Description of a new Crustacean from the Upper
Silurian of Georgia, with Remarks Tipe Calymene Clintom. ,8vo.
Philadelphia, 1880.
Vogt, C. Archeopterya macrura, an intermediate Form between
Birds and Reptiles. Translated by Prof. A. Newton. 8vo. Cam-
bridge, 1880.
Vom Rath, G'. Mineralogische Mittheilungen. Neue Folge. 12. Die
Quarzkrystalle yon Zoptan in Mahren. 13. Ein neuer Beitrag
zur Kenntniss der Krystallisation des Cyanit. 8vo. Leipzig,
1880.
——. Vortrige und Mittheilungen. 8vo. Bonn, 1880.
. Ueber einen sehr kleinen schwarzen Krystall wahrscheinlich
yon Orthit. 8vo. Bonn, 1881.
. Ueber das St. Gotthardgebirge und die Gotthardbahn. vo.
Bonn, 1881.
. Ueber einige neue oder seltene Mineralvorkommnisse. 8vo.
Bonn, 1881.
Waagen, W. On the Geographical Distribution of fossil Organisms
in India. (Translated by &. B. Moote.) Svo. Calcutta, 1878.
Wagener, G., and kK. Krpping. On a new Seismometer, with a
Summary of Observations. 4to. Tokio, 1880.
Wallich, G. C. On the Origin and Formation of the Flints of the
Upper White Chalk; with Observations upon Prof. Sollas’s Paper
in the ‘Annals and Magazine of Natural History’ for December
1880. 8vo. London, 1881.
Wardle, T. The Wild Silks of India, principally Tusser. Folio.
London, 1880.
Warring, C. B. The three Climates of Geology. 8vo. Philadel-
phia, 1880.
Waters, A.W. Quelques roches des Alpes vaudoises étudiées au
VOL. XXXVII. 2a
314 ADDITIONS TO THE LIBRARY.
microscope. 8vo. Lausanne, 1880. Presented by Prof. E. Rene-
vier, F.C.GAS.
Wiebel, K. W. M. Die Insel Helgoland. Untersuchungen iiber
deren Grosse in Vorzeit und Gegenwart vom Standpunkte der
Geschichte und Geologie. 4to. Hamburg, 1848. Purchased.
Wigan Free Public Library. Reference Department. Index Cata-
logue of Books and Papers relating to Mining, Metallurgy, and
Manufactures, by H. T. Folkard. 8vo. Southport, 1880.
Wigner, G. W. Sea-side Water: an Examination into the Character
of the Water Supply at the Watering-places of England and Wales.
Svo. London, 1878. Presented by W. Whitaker, Esq., F.GS.
Williams, J. J. The Isthmus of Tehuantepec: being the Results of
a Survey for a Railroad to connect the Atlantic and Pacific Oceans,
made by the Scientific Commission under the direction of Major J.
G. Barnard; with a Résumé of the Geology, Climate, Local Geo-
graphy, Productive Industry, Fauna and Flora of that Region.
8vo. New York, 1852. Purchased.
Wilson, E. Introductory Lecture on Geology. 12mo. Nottingham,
1872. Presented by W. Whitaker, Esq., F.GS.
Wolf, H. Begleitworte zur geologischen Gruben-Revier-Karte des
Kohlenbeckens von Teplitz-Dux-Briix. S8vo. Vienna, 1880.
Purchased.
Wood,C.J. Tunnel Outlets from Storage Reservoirs. 8vo. London,
1880. ,
Woodward, H. A Catalogue of British Fossil Crustacea, with their
Synonyms and the Range in Time of each Genus and Order. 8vo.
London, 1877. Purchased.
Woodward, H. B. A Sketch of the Geology of Kent. 8vo. London,:
1881 (?).
The Origin of Mountains. 8vo. Birmingham, 1881.
Zittel, Karl A. Handbuch der Paliontologie. Band I. Lief. 3. 8vo.
Munich, 1880. Purchased.
——. ——. Band II. Lief. 2 (unter Mitwirkung von W. P.
Schimper). 8vo. Munich, 1881. Purchased.
——. Ueber den geologischen Bau der libyschen Wiiste. 4to.
Munich, 1880. Presented by the Munich Academy.
35. Mars &e.
The names of Donors in Ltalies.
Belgium. Commassion de la Carte géologique de la Belgique. Carte.
Planchettes Aerschot, Anvers, Beveren, Boisschot, Boom, Heyst-op-
den-berg, Lierre, Lubbeck, Malines, and Putte. 1880 & 1881.
ADDITIONS TO THE LIBRARY. 315
Botella y De Hornos, Federico De. Mapa geologico de Espana y
Portugal. La parte geogrifica por Francisco Coello. Escala de
somo): Madrid, 1879. Purchased.
Dépét dela Marine. Twenty-nine charts and plans of various coasts
and ports.
Figari Bey. Etudes gcographiques et géologiques de l’Egypte, de la
péninsule de lArabie Pétrée et de la Palestine. 1864. (Six sheets.)
Presented by H. Bauerman, Esq., F.GS.
Finlands geolog giska Undersoking. Kartbladet No. 2. 1880.
France. Carte géologique detaillée de la France. Feuilles 9, 23,
34, 50, 67, 69, 78, 93, 113, 122, 213 bis, 225 bis, 237. Scale sou"
1880. Purchased.
Jack, R. L. Geological Sketch Map of the district between Charters
Towers Goldfield and the Coast. Brisbane, 1878.
Ordnance-Survey Maps. Presented by the First Comnussioner of
Works.
One-inch General Maps.
England and Wales. (New Series.) Quarter sheets 269, 284,
301, 308, 314, 319, 329, 332, 333, and 334.
Treland. Hills. Sheets 115, 140, 141, 160, 171, 184, 186-
189, and 194.
Scotland. Hills. Sheets 37, 53, and 103.
Six-inch County Maps.
Argyll. Sheets 70, 85, 97, 129, 137, 148, and 159.
Ce
a (Isle of Canna.) Sheet 53 and 54.
. (Isle of Coll.) Sheet 21.
45 (Isle of Colonsay.) Sheet 145.
an (Isle of Muck.) Sheet 74.
a (Isle of Mull.) Sheets 39, 53, 108, and 109.
. (Isle of Oigh-sgier.) Sheet 64.
(Treshnish Isles.) Sheet 80.
Cheshire. Sheet 2.
Denbigh. Sheets 3, 4, 6, fe 1 LU, | 12 Bay PE Wo. Ak, aici, Se).
——
ead sy and 4H and 46.
Essex. Sheets 1-8, 10-12, 18, 19, 22, 29, 31, 38-40, 42,
45, 46, 48, 56, 58, 61-64, 69-72, 78, and 86.
Flint and Denbigh. Sheet 7 and 8.
Inverness. (Barra.) Sheets 59, 65, 68-70,
3 (Isle of Burra.) Sheets 66 and 67.
. (Isle of Harris.) Sheet 26. —
So
He (Isle of Skye.) Sheets 6, 8-12, 14, 22, 32 and 32,
42, 48, and 58.
- (North and South Uist.) Sheets 24, 25, 32, 36,
41, 54, 56, and 61.
Orkney and Shetland. Sheets 1, 6, 9, 10, 23, 26, 27, 28, 30,
31, 33, 34, 36, 37, 38; 44, 49, 50, 54, and 58.
3216 ADDITIONS TO THE LIBRARY.
Ross. Sheets 27, 5°, 10, 11, 113, 18, 18% 24, 27, 30, 38, 39,
AO, 43; 66,91) 917. 1002 10225 176 22 26) eos
and 134.
Ross and Cromarty. Sheets 5, 16, 17, 25, 26, 41, 52-55,
pee
a ee
65, 76, 77, 67 and 79,92, 93, 101; 104, 1091097 andialias
MO; DIL, 116, 113,119) 120, 123, 124. 1285 tiene
—V—$—$———
and 133 and 130.
Ross, Cromarty, and Nairnshire. Sheet 89.
Surrey. Sheet 3.
Sussex. Sheets 11, 13, 22, 34, 36, 47-49, 61, 62, and 66.
: ti
Wilts and Hants. Sheets 76 and 54.
Preussen und die thtiringische Staaten. Geologische Specialkarte.
Gradabtheilung 67, Nos. 53, 54, 59, & 60; Gradabtheilung 68,
Nos. 49 & 55; und Gradabtheilung 80, Nos. 19, 20, 25, 26, 31,
& 32. 1889. Presented by the Prussian Ministry of Manufac-
tures, Trade, and Arts.
Saxony. Geologische Landesuntersuchung des Komgreichs Sachsen.
Geologische Specialkarte. Blatt 28, Grimma; Blatt 75, Langen-
leuba; Blatt 115, Zschopau. 1880.
Sheafer, Messrs. Diagram of the Progress of the Anthracite Coal
Trade of Pennsylvania, with Statistical Tables &&. 1879. Pre-
sented by P. W. Sheafer, Esq.
—. ——. Presented by Dr. F. V. Hayden, PMLGS.
Siedamgrotzky. Flotz-Karte des Aachener Steinkohlen-Beckens.
Scale sa" In 7 sheets. Purchased.
Switzerland. Commission géologique pour la Carte géologique de la
Suisse. Carte géologique, feuilles I1V.& V. Scale jou
Wolf, H. Geologische Grubenrevier-Karte des Kohlenbeckens von
Teplitz-Dux-Briix im nordwestlichen Bohmen. Blatter 1-16.
Scale .+,. Vienna, 1880. Purchased.
Il. ADDITIONS TO THE MUSEUM.
Specimens of Carboniferous Limestone Fossils from Flathead River,
Rocky Mountains, 49th parallel, N.W. America. Presented by H.
Bauerman, Esq., F.GS.
The Type Specimens of the “ Tubulations sableuses ” of the “ Etage
Bruxellien ” from the environs of Brussels, descrihed by H. ./.
Carter, Esq., in the ‘Annals and Mag. Nat. Hist.’ for May 1877.
Specimens of Tertiary Palliobranchs from South Australia, and three
specimens of Belemnites from Central Australia. Presented by
Prof. 2. Date, H.G.s:
y 1442 ©
o<}s
7s
a
> ive
TT
Live Music Archive
Librivox Free Audio
Metropolitan Museum
Cleveland Museum of Art
Internet Arcade
Console Living Room
Books to Borrow
Open Library
TV News
Understanding 9/11