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THE

QUARTERLY J OURNAL

tEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

Quod si cui mortalium cordi et curs sit non tantum inventis herere, atque iis uti, sed ad ulteriora
1etrare ; atque non disputando adversarium, sed opere naturam vincere ; denique non belle et probabiliter
mari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant
Novum Organum, Prefatio.

ern Ho Tipo
HAIN MISTI
‘Cy
%

24a

Wc
<Xy*
¢ Ase
2h Na kh ps RMR
PART THE FIRST.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

VOLUME THE TWENTY-S&
1866. |

LONDON:

LONGMAN, GREEN, READER, AND DYER.

\RIS;—FRIED. KLINCKSIECK, 11 RUE DE LILLE; J. ROTHSCHILD, 14 RUE DE BUCE.
LEIPZIG, T. 0. WEIGEL,

SOLD ALSO AT THE APARTMENTS OF THE SOCIETY.

MDCCCLXVi.

Ltst
OF THE

OFFICERS

OF THE

GEOLOGICAL SOCIETY OF LONDON,

PIPL ELI DDSI

Elected February 16th, 1866. .

Present.
Warington W. Smyth, Esq., M.A., F.R.S.
; Cice-Jrestvents.
Sir P. de M. G. Egerton, Bart., M.P., F.R.S. | Sir Charles Lyell, Bart., D.C.L., F.R.S.
- Prof. T. H. Huxley, F.R.S. & LS. Prof. A. C. Ramsay, F.R.S.
| Secretartes.
P. Martin Duncan, M.B. ‘ | John Evans, Esq., F.R.S., F.S.A.

Foreign Secretary.
R. A. C. Godwin-Austen, Hisq.) Rese

Treasurer.
_ Joseph Prestwich, Esq., F.R.S.

COUNGEIL.
H. W. Bristow, Esq., F.R.S. . Sir Charles Lyell, Bart., D.C.L., F.R.S.
P. Martin Duncan, M.B. John Carrick Moore, Esq., M.A., F.R.S.
Sir P. de M. G. Egerton, Bart., M.P., F.R.S. | Prof. John Morris.
Earl of Enniskillen, D.C.L., F.R.S, : Sir R. I. Murchison, Bart., K.C.B., F.R.S.
R. Etheridge, Esq., F.R.S.E. Robert W. Mylne, Esq., F.R.S.
John Evans, Esq., F.R.S., F.S.A. Joseph Prestwich, Esq., F.R.S.
R. A.C. Godwin-Austen, Esq. Panes. Prof. A. C. Ramsay, M.A., F.R.S.
William John Hamilton, Esq., F.R.S. Warington W. Smyth, Esq., M.A., F.R.S.
Prof. T. H. Huxley, F.R.S. & LS. | Capt. T. A. B. Spratt, R.N., C.B., F.R.S.
J. Gwyn Jeffreys, Esq., F.R.S. Lieut.-Col. R. Strachey, R.E., F.R.S. & L.S.
Prof. T. Rupert Jones, Rev. Thomas Wiltshire, M.A., F.R.A.S.

M. Auguste Laugei.

Assistant-Secretary, Librarian, and Curator.
H. M. Jenkins, Esq.
Clerk.
Mr. P. G. Ritchie.

Libvary and PAuseum Assistant.
Mr. R. Tate.

PP eee eee MUM Re AS6 Bk Sh me Fe we 6 te Se Oe MS ee We oe On Te

TABLE OF CONTENTS.

PART I,—ORIGINAL COMMUNICATIONS.

Page
Apams, Dr. A. Lerru. On Fossil Chelonians from the Ossiferous
(eres-eud Wissures of Malia ..... 6s .cerscevennerpenvnovsos 594

BaveErMAN, H., Esq. On the Copper-mines of the State of Michi-
nga yp kg ek riae Cag tae eg Wee nsaegunes s 448

Brine, Commander L. On. the recent Volcanic Disturbances at
UM USMC ogres ceded rrkier eee ¥ eer trebaretees 318

Bristow, H. W., Esq. On Supposed Remains of the Crag on the
North Downs near Folkestone .......,.ssss085 Siaee gt Uheieace 553

Broprk, Rev. P. B. Ona Section of Lower Lias and Rhetic Beds,
NR OMRCPCES cs ss oak ho pre pec PEO e oR be Bae beat

CARPENTER, Dr. W. B, On the Structure and Affinities of Hozodn
ME eT a rien Sse E Ra g's re Coe hk LOM oe Re One erh eae

CUS pS TS ee es a ce

Dawetns, W. B., Esq. On the Fossil British Oxen. Part I. Bos
(OEE REA DIMES gg al eee apg ge clot oe A oes an 391

On supposed Burrows of ‘Worms in the Laurentian Rocks
Te Ee bene og #35 cake Brak too F Lee Goeees ees 608

Dawson, R., Esq. On the Occurrence of dead Littoral Shells in the
Bed of the German Ocean, forty miles from the Coast of Aber-
deen. [Abridged.].s.sscasseeeneeees 5 ape Al oe ae rer 260

iv TABLE OF CONTENTS.
Pa
Décrgata, M. On the recent Volcanic Disturbances at Santorino. a
[-Asbstiact:]] . . sues sie deine MRS. soar eee 25S syne eis . 318

DELENDA, A., Esq. On the recent Volcanic Disturbances at Santorino
[Abstract.] 5 2., 0 Ea Gee co 2 318

Duncan, Dr. P. Martin. On some Spaces formerly occupied by Se-
lenite, in the Lower Eocene Clays of the London Basin; with
Remarks on the Origin and Disappearance of the Mineral .... 12

Eerrton, Sir P. de M.G. Ona New Species of Acanthodes from
the’ Coal-shales of Longton. (With 1 Plate,)). . Saas enneee 468

Fisumr, The Rey. O. On the Relation of the Norwich or Fluvio-
marine Crag to the Chillesford Clay or Loam ..... cin ene

On the Warp (of Mr. Trimmer)—its Age and probable
Connexion with the Last Geological Hvents. [Abridged.].... 553 ,

Fiower, J. W., Esq. On some Flint Implements lately found in
the Valley of the Little Ouse River, near Thetford. [Abstract.] 567

Fovugut, M. On the recent Volcanic Disturbances at Santorino.
[Abstracts] oc. vs ccne ness sec eeeess su eos sce ofes ter , 318

Gopwin-AvsTen, Capt. H. On ihe Carboniferous Rocks of the
Valley of Kashmere; with Notes on the Brachiopoda, by T.

Davipson, Esq., F.R.S., F.G.S. (With 2 Plates.) ........0s 29
Gapwin-AvustEn, R. A. C., Esq. On the Submerged Forest—beds
of Porlock Bay eo ceo oo ee reo eee eee eeesoesev ose Oe

On the Kainozoic Formations of Belgium.........+. ‘spin eae
Guppy, R. J. L., Esq. On the Tertiary Mollusca from Jamaica.

CWith 3 Plates.) 0.) i.e cccea ws ao sie eee + onellsh er 281
On the Tertiary Brachiopoda from Trinidad. (With part

of We Rlaten) eae etre eee ‘sles ba aloes pie 6 0 ain eh eis 295

. On Tertiary Echinoderms from the West Indies. (With _

PArh Ox A Plat.) nce as sie-ea.sin «oleh serene MP yu 297

On the Relations of the Tertiary Formations of the
West Indies; with a Note on a New Species of Ranma
from the Tertiary Strata of Trinidad, by H. Woopwarp, Ksq.,
F.G.S8.; and a Note on the Orbitoides and Nummuline of the
Tertiary Asphaltic Bed, Trinidad, by Prof. T. R. Jonzs, F.G.S.

CAN tL Plaite ich waters hs Sie oa: @ vacnieie abel oReien a ee ee
Harxyess, Prof. R. On the Metamorphic and Fossiliferous Rocks
of the County of Galway .........06. veeseee si9 aa) oem . 506

, and H. Nicrorson, Esq. On the Geology of the Lake-
country ; with a Note on Two New Species of Trilobites, by
J. W.. Salter, Esq. Ac LiS., BGS... cece 480
. On the Lower Silurian Rocks of the Isle of Man 488

y)

TABLE OF CONTENTS. Vv

Pa
Hoiiand, The Rey. F. W. On the Geology of Sinai. [Abstract.] 491

Hueuss, T. M‘K., Esq. On the Junction’of the Thanet Sand and
the Chalk, and of the Sandgate Beds and Kentish Rag........ 402

Jamirson, T, F., Esq. On the Glacial Phenomena of Caithness..., 261

Juxss, J. B., Esq. On the Carboniferous Slate (or Devonian Rocks)
and the Old Red Sandstone of South Ireland and North Devon 320

Kerns, W. Esq. Onthe Brown Cannel, or Petroleum, Coal-seams

at Colley Creek, Liverpool Plains, New South Wales........ 435
Kine, Prof. W., and Prof. T. H. Rowney. On the so-called Eozoonal

EBC: or ies wiaes tus civnesvapaetessseave 185
Luoyp, St. V., Esq. On the Recent Volcanic Disturbances at San-

SP EMALIASEDC DT dk s bic klsireiSal bie d aides ewan’ Del wan ded cee 318
Locxr-Travers, W. T., Esq. On the Formation of Lake-basins in

ery a: ai ela id seid Wathiard #06 Wee's alse a aieae a'eed eves 254
Neate, Lieut.-Col. E. St. J. On the Discovery of New Gold-depo-

sits in the District of Esmeraldas, Ecuador.............5. «ve, 098

Pixr, J. W., Esq. On some remarkable “ Heaves” or Throws in
NIM oS Nai a. «Hides Cale gs a MOSER EW Dae ea R Es 535

PLANT, Z Esq. On the Discovery of Primordial Fossils in the
Lingula-flags in the Neighbourhood of Tyddyngwladis Silver-
MAES CUSEURCE. | Wells sk u.0'v aid a eens es ce mcien ce aees ean 505

SALTER, J. W., Esq. On Faults in the Drift-gravel at Hitchin, Herts 565

SEELEY, H., Esq. On the Gravels and Drift of the Fenland.
OS Sener ACRE hc See ee 470

Tawney, E. B., Esq. On the Western Limit of the Rheetic Beds in
South Wales, and on the Position of the Sutton Stone; with a
Note on the Corals, by Dr. P. Martin Duncan, Sec. G.S.
ECCS) ru fe b.u04:0 4 a> e405, 0'0 0.4)a 6 heen ORIGIN aun, etal n a S's 69

Tryon, Commander G. On the recent Volcanic Disturbances at San- ©
UME OPEB [yaa eas, + « 6. ova ¥ windo's'v evtaety soe De ee OS es 5 318

Tyxor, A., Esq. On the Interval of Time which has passed between
the Formation of the Upper and Lower Valley-gravels of Eng-

MESO 0a uiclycsisuiunia Reddy Chae mee ewe bike ek 463
Watson, The Rey. R. B. On the Marine Origin of the Parallel
Roads of Glen Roy. [Abstract.]...... Sein xo auek'e 2 eee

Wuitaker, W., Esq. On the “Lower London Tertiaries” of
Mento CWith 1 Plate.)vce ss ost eens Sino NG oo a'r 6/0 vate 404

Witiiamson, Prof. W. C. Ona Cheirotherian Footprint from the
Base of the Keuper Sandstone of Daresbury, Cheshire. [ Abstract. ] 534

Woop, 8. V., Esq. Onthe Structure of the Red Crag ....0.0++, 588

V1 TABLE OF CONTENTS.

Page
Woopwarp, H., Esq. On the oldest known British Crab (Palei-
nachus longipes) from the Heese Marble, Malmesbury, ee
(With part of 1. Plate.) ...scccetecss cus sve seur reeset ees 493

. On the Species of the Genus ZEryon, Desm., from the Lias
“and Oolite of England and Bavaria. (With parts of 2 Plates.) 494

. On a new Genus of Phyllopodous Crustacea from the
Moffat Shales (Llandeilo Flags), Dumfriesshire. (With part of

L Plate) Pia eee eee sree hs Pee ee ee 503.
Youne, Dr. J. On the Affinities of Platysomus and ge. genera.

CWith? Plates. erie ice etaisicia asians owe siatae OOL
——. On the Scales of Rhizodus, Owen. [Abstract.]....+.0:+5 817
———. On the Affinities of Chondrosteus, Ag. [ Abstract. ie Pviearee 596

——.. On New Genera of Carboniferous Glyptodipterines ....,. 596

Annual Report ee OTE SE OC En ceo cue ak i

Atiniversary Address sssisiisaseteisisisiaesaittstaaepein xxvii
List of Foreign Membersiiit.stiatiaiiiastvads sassobeaevene) Geewaae
List of Foreign Correspondents ..,...:....::. aa) eeeeeee xix
List of the Wollaston Medalists iiicicacscisacestestasetenee KX

Donations to the Library (with Bibliography) .... x, 46, 170, 372, 610

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.

PLANT (71).

Alethopteris grandis, P\.xiii.f. 100. Bay de Chaleur..| 157
Antholithes pygmea. P\. vii. f. 30¢ JOZPINS ....5.088 149
— Rhabdocarpi. PI. vii. f. 30.... Grand Lake...... 149
—— sguamosa, PI. vii. f. 29....... PictOW savescadee 150
Araucarites gracilis. Pl. vi. f.14.. Tatamagouche...| 146
Asterophyllites trinervis. P1.xiii.f.90 Sydney... .cscaass 152
Grand Lake,

Beinertia Gepperti. Pl. xiii. f.101. Bay de Cha- ! 159

leur, Joggins

BEMMPUNURBOUEUN MUIR TCO sheccccscsee | | cu ess PP eabeteseeticces beens
ai Nova-scotica. Pl.xii. f. 89... Joggins ...06...) 151

amodendro roximn : ‘
2 Py OBEY; TORRIBR |. ake
— obscurum. PI. vii. f. 31d...... | Sydney...... dsasael > 149
Cardiocarpum bisectum. P1.xii.f.73 Grand Lake......| 165
— fluitans. Pl. xii. f.74 ......... JORSING sicscaavs 165
Ciathratia. Pl. Vii. £28 «:::........ Nova Scotia......| 130
:
Cordaites simplex svaaade SER UU ge cess f Coal-formation Hee } 164
p j gai Horton, Nor-
Cyclopteris Acadica. PI. viii. f. 32... { ta Eeeelk si 153
— antigua. Pl. xiii. f. 95......... Hebert River ...{ 154
— hispida. PI. xiii. f.92 ......... Sydney........006. 154
Dadoxylon Acadianum. Pl.v.f.4,5,6 || JOSRINS seeesseas 145
annulatum. Pl.v.f.10-13 ... | JOPPINS. ..eessaee 146
— antiquius. Pl.v.f.1-3......... Hortonisasicsisss. 146
—— materiarium. Pl.v.f.7-9 ... Joggins, Pictou | 145
Diplotegium retusum. P1. xiii. f. 102 JOZPINS, vassvese, 164
Equisetites curta. Pl. xii. f. 88...... SYGHEY..sicissasus 151
Pavuiatite: Pl. Vil fe 26,27 © coccccses | Nova Scotia...... 130
Hymenophyliites pentadactyla ..... . YORE V rc easeces. 159
eee corrugatum. P1.xi. | Pare ees.) ed
—— decurtatum. Pl. ix. f.40 ii... Pietow sy iisisissce. 161
personatum. Pl, ix.f.39 ...... Sydney....e-sssees 162
— Pictoense. Pl. ix. £.37....0004-

Sydney, Pic-
tou, Grand 161
\ | Lake.

vill

Name of Species. | Formation. | Locality. |Page.

PLANT (continued).

Lepidodendron plicatum. PI. ix. £.39 \ ( PictOW “.eee eee
Lepidophloios Acadianus. P\.x.f.45, ;
Phe Col eae ae Foggins, Sydney
Pictou, Jog-
POTCUs. PAA sie Otaoscets soe ae Sy ES. é
platystigma, Pl.x. f. 47, 48... Sydney, Joggins.
prominulus. Pl. xi. f.52 cis. Jogeims < recsctee
tetragonus. Pl.x.f.49 ...... Jogging ase ms
Lepidostrobus longifolius .........00 JOGSINS 00. --nee
squamosus. Pl. x. f.46 ....... Grand Lake......
Lonchopteris tenuis. Pl. xiii. f. 103 Sydney asco neeeee
Megaphyton humile. Pl. viii. f. 33.. Sydney...- 6 vee
magnificum. Pl. viii. f. 34 ... | JOPZINS ...000...
Neuropteris cyclopteroides. PI.
Eis ee ea | SYOn ge
perelegans. PI. xiii. f. 93....... SYQNEY aeaeeenen
Negyerathia dispar. PI. xiii. f. 91.. Bay de Chaleur...
Paleopteris Acadica. P\. viii. f. 36.. PictOu (comer eee
GTAP SAMI OD cee Grand Lake......
WPCCODTENIS: TAGLAG Manian dos. 6 doles setae PiCtOul tema eee
Phyllopteris antiqua. Pl. xiii. f. 96 SYGney.as..ewene
PERNUIATIG CROSS Gee sess te Neral jana Horton...
Ratieceinsinsie, Patt lo maton 1
Sigillaria Bretonensis. PI. vii. f. 27 NY CNEY se uceeeeeeee
Brownii. Pl. vi. f. 15-19...... JOggINS ser...
catenoides. Pl.vi.f.22 ...... Joggins, Sydney.
elegans... (Ric vit. £26 2 w.neess: Joggins, sven
eminens..” Pliyict..24) .oscscss VOMeVacaen seas
——— planicosta. Pl. vi.f.21 ...... | Sydney... cece me
scutellata, Pl wit f.120....ccce. JOS SINS omelet
striata. PlNi M2 on casisasexs | Joggins “sen-ae
Sydnensis. Pl. vii.f.28 ...... Sydney......c0e. 5c
Sphenopteris Canadensis. P\. xiii. { Bay de Cha-
Ja Oh sasanas Haganeadscabonunarecsndec } leur, Sydney ?.
lation. Pl, xiii. £.98....c.000 | Bee
MUNA. © EV exanit. 97 see ercccwsie. Grand Lake......
Sporangites glabra. Pl. xii. f. 81... JOGO INS araeeeetes

papiulata. wr lexiettO0 Weseccer JOS PINS Vee aweeeet
Stigmaria ficoides. Pl. xii. f. 83-87 Hortou, Sydney..
Trigonocarpum avellanum. PI. Joggins, Syd-

POLL ce sdid. a altane vse nee eeee eee wears Ney sh ieceae

intermedium. PI. xii. 78 0.45. | Joggins iieeese
—— minus. PI. xii. f. 75 .........008 Joggins ......0..
LOUMIUGAURIC ©, Setlaaislelscisaiseicises cia sles's JOgeins vases
— Sigillarie. Pl. xii. f. 76 a ieeee | Jogeins jvanseeus
Protozoa (1).
( Rhizopoda.)
Eozoon Canadense.s......- scocsveoeceess-(LAULENGIAN 4... ++-|CAMAAA...00re0srae0e}
EcCHINODERMATA (3).
Echinolampas lycopersicus. P1. xix. ee Anguilla ...... sist
ovum-serpentis. PJ]. xix. f. 4-6... + |Tertiary .,.... Trimidad Wesco
—— semiorois. JRA xe f. Citiisonesinenes | Anguilla dovveceee

300

1X

Name of Species. Formation. Locality. Page.

Motuusca (108).

- (Brachiopoda.)

Athyris subtilita, var. Pl.ii.f. 2... (Kashmere ......| 40
Chonetes? Austeniana. P1.ii.f.18.. Kashmere ...... 44
Hardrensis, var. | Thibet 36

Pr ikea | {es ll pee
CD Ae oy eee Kashmere ...... 44+
Discina Kashmeriensis. PI. ii. f. 19 Kashmere ...... 45
A Eg Se ab re TAGE ois icon cant 36
Productus Humboldtii. Pl. ii. f.13 }|Carboniferous .../¢ Kashmere ......) 43
— levis. Pl.ii. f£.16........0008- - Kashmere ......| 44
— scabriculus. Pl.iif.13 ...... Kashmere ......| 43
— semireticulatus. Pl.i.f.6 ... EHIME cts sesonsne 36
— PME ES | cxasenncsace Kashmere ...... 43
spinulosus? Pl.ii. f.15 ....0. | Kashmere ...... 44.
Rhynchonella Barumensis. P1.ii.f. 8 Kashmere ...... 42
Kashmeriensis. Pl.ii.f.9 .../) Kashmere ...... 42,
Merumense PIL1.£.15,16 ....../JUrassiC ...c0c000) 1 MIDEE ........00c.00- 37
adil cena Carboniferous ...|Thibet ........+.+« ale 36
eae tet. fo 9, 10... ces cncas ere Cretacis viens] PaiDeE Soo) oie ce conse 38
Spirifera Barusiensis. Pl.ii.f. 7...) (Kashmere ...... 42
Kashmeriensis. Pl.ii.f.5 ... | Kashmere ...... 4]
— Moosakhailensis. Pl.ii. f. 6... Kashmere ...... 41
Be PLIES. ccvercceveeys Kashmere ......| 40
— Vihiana. Pl. ii. f.4 wreccocesese Carboniferous ...|4 Kashmere ...... 41
——, Sp. PLif.d ....rcccccseceees EDWeE «KR ....c05: 36
Streptorhynchuscrenistria. P1.ii. f. 10 3 Kashmere ..... 3
2 Se 2D) | Kashmere ...... 43
Terebratula Austeniana. PI. i. f. 1 \ Thibet ............ 30
er} Dertiony s.sessssf Trinidad wai, 296
SIGRCOUMISs Pls 11 f. 1 .....cccccccees Carboniferous ...|Kashmere .......+. 40
— Thibetensis. Pl.i.f. 11-14 ...... JUEASSIO S656 05% THIDEE ceases omcsnne’ 37
ivuatatensis. P\. xix. f. la, 6...|Tertiary .......0./Trinidad ,...0.00e00. 296
— et Cretaceous ......|Thibet ...sersererss.. =

(Lamellibranchiata.)

Anatina precursor, var. Pylensis Pl. Ae | Pyle, Stormy 88

ES G2 Se Wee sandstones ... De Wit) ee nase
Anomia socialis. Biase lO». cect: Sutton Series .../St. Mary Hill ...... 85
Arca filicata. Pl. xxvi.f.5 ......... Trinidad .........] 983
inequilateralis. Pl. xviii.f. 2 +|Miocene ..... ../) Jamaica ........ 293
— Trinifaria. Pl. xxvi.f.3...... "EEMGIGAG ohcne anc 583
Astarte Duneani. Pl.iv.f.4 ...... 87
ee, Rag aa Sutton Series .,.|Suttom ssovsessessseos a
Cardita? rhomboidalis. PI. iv. f. 6.. 87
scabricostata. PI. xviii. f. 10. \ Jamaica ....0... 293
Cardium castum. Pl. xxvi.f.4 ... | TEimMidad: ...c0cecs 582
—— inconspicuum. Pl. xviii. f.7.... $|Miocene ys. Jantatea vcccanns 293

lingua-leonis. Pl. xviii. f. 7... ie QMIDICH: zien 293
Ceromya ledeformis. Pl. xxvi. f. 1.) Trinidad ...... v| oO8l

x

Name of Species. . | Formation. | Locality. |Page.

Mottusca (continued).
Lamellibranchiata (continued).

: Trinidad eases
Corbula vieta. Pl. xxvi. f. 8......... Miocene ......... JAMBIC2, apneaeee 581
PHOCENC ayo sy 3 Trinidad .pesexscsses
wiminea. P\, xvii. f. 11. 2..°..... Miocene ........- JaMaicay ih seca reas ane
Cyprina normalis. Pl. iv. f. Z....-0000. Sutton Series ,../SUttON,..3.,:peunseee ee
Cytherea (Circe) carbasea. Pl. xviii. \

(ie (Rypranceadrionseaicn. jooan wooded aodbodts Jamaica ...... sel eve
juncea. Pl. xxvi. f. 13. Cumana ........| 582
(Calista) planivieta. PI. ‘xviii. \ Miocene .....««+.| 4

Bit bragéndsosdsanSonocer nae pecnennanders JAMAICA, eseeeeees| OZ

Erycina tensa. Pl. xxvi. f. he ceeaials Trinidad: «asce) 582
Gryphea athyroides. Pl. xxyi. f.17. ) \ Trinidad s.sccpegs| 0Bbe
Lima angusta. Bl st oOs, casa sacar autpan series ...\Sutton, Dunraven..| 83

utton & South-
Dunravenensis. PI. iii. f. 9.. 4 pabelgtin SeHAS. } Dunraven eteeee 84
planicostata, P\, ii. ts Zoscesse so Sutton series .../Laleston, Sutton...) 83
subduplicata. Pl. iii. f. 8...... Sutton & South- { SULtON srssreaee (syle
bubereulata Cp aseeya-eescsscs sen erndown series.| | Bridgend......... 82
Mactrinula macescens. Pl. xxvi. f. 2.|Miocene ......... Trinidad: yi checyssuss 581
‘Modiola imbricato-radiata. Pl.iv.f.8. . SUttON ccppare< sees 87
wOstren Wevis. .9P I. Vis Aen ssengnen saudnee Sutton, Langan 84
Ostrea multicostata. PI. iii f. 1.... | |Sutton & South-| | Sutt 84
Pecten Etheridgii. PA. iii. f. hae erndown series. } OR epee ver ae 81
meequalis, Bly xvas f.Oces sce Tertiary ses. pcece JAMAICA soepeoneencl Ot
Suttonensis. PI, iii. f. 3....... Rens Souths eee ieee 82
Pinna insignis. Pl. iii. £. 5. ......00 erndown series. i sy, BD: | 85
; es Southerndown
Berna © RGMSAYlovebe saan sero Agno too We hea ek Near Sutton ... 86
Venus Walli. Pl. xxvi. f. 16. ...06 \ Miacene eee siepebeeeh TE
Woodwardi. P\. xviii. f. 1.... meee | | SA e eee ee
(Gasteropoda.)

Ancillaria lamellata. P\. xxvi. f. 9. \ (\Trinidad ...,,..»0s9| 579
Cancellaria Barretti. Pl. xviii. f. 11. (289
—— levescens. Pl. xvii. f. 12...... | 289
Mooret. Pl. xvil, f. 7+ ...0r009% 289
Cassis monilifera. Pl. xvii. f. 8. | 987
Cassidaria sublevigata. Pl.xvii.t. 10. | 287
Cerithium plebeium. PI. xvi. f. 9... | | 290
Columbellaambigua. P\. xvi. f. 8... | 288
gradata, Bi. xvi; £10 oe ss0re | ; 288
Conus gracilissimus. PI. xvi. f. 4... }|Miocene ...... { Jamaica .........4., 288
granozonatus. Pl. xvi. f. 5...... | 287
— interstinctus. Pl. xvi.f. 3. ... | 288
planturatus, Plex. £7... 287
—— solidus. PJ. xvi. f.1............ | | 287
stenostoma. Pl. xvi. f. 2....... | 287
-Clyclostrema bicarinata. Pl.xvi. f. 5. a 291
Dentalium. dissimile. Pl. xvii. f. 4. | 292
Fasciolaria semistriata. Pl. xvi. f. ] 2 | 288
Ficula carbasea. PI. xxvi. f. 7., Trinidad, Anguilla} 580
Malea camura. Pl. xvii. f. 9. whit 287
Marginellaconiformis. Pl.xvii.f. 2. ammiene 288
Melanopsis capula. Pl. xxvi. f. 14 C 280
Nassa solidula, PI. xxvi. f. 11... emmmineie .

Natica phasianelloides. Pl. xvii. f. 1) Jamaica wesc] 201

x
Name of Species. | Formation. _ | Locality. | Page.

Mot.usca (continued).

Gasteropoda (continued).

Natica Pylensis. Pl.iv. f. 10. ...... Avieula-contorta| | Pyle, Stormy } 89

sandstones. ... DOWD. ...<c00s
— subclausa. PI. xviii. f. 8....... 290
— suleata. PI. xviii. f. 14, 15.... }|Tertiary ...... pon PAMGICA Sv atane devant oO
Neritina Woodwardi .........reecceuee 291
Patella Suttonensis. P1. iv. f. 9a, 6....|Sutton series ...|Sutton....... neem 88
Persona simillima. PI. xvii. f. 13... ) 288
Phos elegans. Pl. xvi. f. 13 ......... ! 290
Weoerer.) El. xvi. f. 11 ........ Jatnice 290
Pleurotoma Barretti. Pl. xvii. f. 6. Ree 290
Jamaicense.. Pl. xvi. f. 6 ....00 2 290
Ranella crassa. Pl. xviii. f. 9 ...... MAIDEN tes esv ees aes

Cumana ......+ ai
Turritella tornata. Pl. xxvi. f. 12. 7 PADMIICD cn cicseon 580

7” { San Domingo ...
Vermetus papulosus. Pl. xvii. f. 3.) | JANBIEA. 6.602000 292

© (Cephalopoda.)
Ammonites Dunravenensis. P1.iv.f.1. . ’ Dunraven
be PE PCBCMIGER, co vsntvevusicsccvecs.cee Sutton nce re 1 Sutton gti | 81
ANNULOSA (13).
(Annelida.)

Annelid-tubes. Wood cuts.cccccces eecees Laurentian OF eoe Canada eeeeesoesees 608
Spirorbis clymenioides. P1. xxvi.f.10.'Miocene .........| Trinidad ...... seoss-| O84
( Crustacea.)

Agnostus Morei. Woodcut, f. a, &. ...|Lower Silurian ..|Near Milburn ...... 487
Discinocaris Browniana. P1. xxv. f.4—7|Moffatt Shales...|Dumfriesshire ...... 503
Mevam Garrovensis. Pl. xxv. f. 1.......[Lias ......c.scce0s- Barrow-on-Soar ...| 496

eames.) Pl. xxiv. f. 2.........008. Lower Lias ...... Lyme Regis......... 498
crassichelis, Pl. xxv. f. 2......... LAGS Neseay saosetens Dorsetshire ......... 497
RMR i. XXV. £. 3. secsvees sons Upper White Lias\Iminster ............,_ 499
—— Oppeli. Pl. xxiv. f. 4. ......... eee \ Solenhofen ...... \ 500
Wilmcotensis. Pl. xxiv. f. 3...... Lower Lias .....: | Wilmcote........ Jew) ¢ 200
Paleinachus longipes. PI. xxiv. f. 1...|Forest Marble ...|Malmesbury. .,,...| 493
Phacops Nicholsoni. Woodcut, f. c, d.|\Lower Silurian ..|Whiteside ......... 486
Ranina porifera. Pl. xxvi. f. 18.......!Tertiary .e...... Memdad: sc ceisennes's: 591
VERTEBRATA (17).
(Pisces.)
Amphicentrum granulosum. Pl. xx....|Coal-measures...|North Staffordshire; 306
Acanthodes Wardi. Pl. xxiii. .....,.../Coal-shales ...... 0) 468
Dendroptychius. Woodcut, f. 7. ...... CarOmirecO sy ce| 2. ecben tans seeniceses vais 601
MRCOG | Soe toc cvs. -ssevencoesncedases Carboniferous ...|Fifeshire ............ 315
Eurysomus (=Platysomus) .........0«+ WOAI-INCHSHBER 0. tevceveeewecs aria assaeu|e. onee
HiGloptychius =.......0060. ssichiduieoaueeesss CarbOmitlerOus) 56 |oss0ce5 «se senas ses cenees 601
Megalichthys eeerocsare Poet eeererteeeacere Carboniferous @erleeecvcece Cen POceoseenees 606

Xl
Name of Species. | Formation. Locality. |Page.

VERTEBRATA (continued).

Pisces (continued).

Mesolepis scalaris s.....000. Use uecanes 314
Ward. Pl, xxtke lerospenpee .. + (Coal-measures...|North Staffordshire] , 314
Platysomus parvulus. PI. xxi. f. 2 303
Rhizodopsis. Woodcut, f. 8............ Carboniferous ...|.. sista stoped siaeeeee popeae 599
Rhizodus. Woodcuts, f. 4,5 ......... Carboniferous: ...\csescs asses ore eeeenee 599
Rhomboptychius. Woodcut, f. 1, 2...;\Carboniferous ...}.........sseseesssseeees 604
Strepsodus. Woodcut, f.3 ....... »..+.(Carboniferous ...|.... disirns sama cosgaeeee | 602
. (Reptilia.)
Chelonians, bones Of ....sseeeceeseeceees-{CAVEINS seareceee| Malta seersesversres: | -594
(Mammalia.)
DOS WUUSccr ees -neavencspeaceno rose xeoeseona | UALCEMATY «9. 7d| teenem bhaacraiobn ac staistonl|) = rehenae
Halitherium. Wood cut....cc....coeeeee NOGEME terse acne Malta vie sean sneer 595

INCERT& SEDIS (1).
Cisseis asteriscus. Pl. xxvi. f. 19......|Miocene .......-/Trinidad we..sss.00| 584

GEOLOGICAL SOCIETY OF LONDON.

ANNUAL GENERAL MEETING, FEB. 16, 1866.

REPORT OF THE COUNCIL.

Tur Council of the Geological Society of London are glad to be able
to announce, in laying their Annual Report before the Fellows, that
a very large addition to the number of Fellows, similar to that
noticed at the close of the last two years, has been made during the
past year.

During 1865 as many as 66 new Fellows were elected ; but of
these only 45 had paid their fees up to the end of the year, making
with 11 previously elected, who paid their fees last year, a total of
56 new Fellows. On the other hand, the numbers of the Society
have been reduced by the death of 17 Fellows, the resignation of 5,
and the removal of 4, giving a net increase of 30 ordinary ‘Fellows.

The Society has recently had to deplore the loss of its only re-
maining Fellow of Royal Blood—the late King of the Belgians.

Four Foreign Members and one Foreign Correspondent have been
reported as deceased.

One Foreign Correspondent was elected during 1865 in the place
of one deceased.

The total number of the Society at the close of 1864 was 1092 ;
at the close of 1865, 1117.

The prosperous condition of the Society is indicated by its increas-
ing Income, as well as by the augmentation in its numbers. The In-
come of the past year has exceeded the expenditure by £268 10s. 3d.,
although the disbursements include the special expenditure on ac-
count of the Bequest-fund for the new edition of the Greenough
Map.

The funded property of the Society remains the same as at the
last Anniversary, namely £4560.

The Council have to announce the completion of Vol. XXI. of the
Quarterly Journal, and the publication of the first part of ee XXII.

MOUs KIT.

li F ANNIVERSARY MEETING.

The New Edition of the Greenough Geological Map was completed
at the commencement of the year; it has already met with a satis-
factory sale, and can be obtained at the Society’s Apartments, or of
the agent, Mr. Stanford.

Among other donations made to the Society since the last Anni-
versary, the Council have to make special mention of a marble bust
of Dr. Bowerbank, F.R.S8., F.G.S., presented, in accordance with his
wish, by the Committeeof the Bowerbank Testimonial Fund.

The Council regret to have to report the sudden death, in December
last, of the Society’s clerk, Mr. G. E. Roberts; they have recently
appointed Mr. P. G. Ritchie to fill the vacant office.

The Council have awarded the Wollaston Medal to Sir Charles
- Lyell, Bart., F.R.S., in recognition of the highly important services
he has rendered to Geology by his various original works, and for
the masterly and philosophic manner in which he has treated the
subject, both in developing the principles and in expounding the ele-
ments on which the Science is founded ; and the balance of the pro-
ceeds of the Wollaston Fund to Henry Woodward, Esq., F.G.S.,
F.Z.S., to assist him in his researches on the Fossil Crustacea.

Report of the Labrary and Museum Committee, 1865-66.
The Museum.

The additions made to the Society’s collections since the last Anni-
versary have not been so numerous as in previous years ; they con-
sist chiefly of specimens of rocks and minerals from foreign countries.
The more important donations are the following :—Ilst. An exten-
sive collection of Rocks and Minerals from Roslagen, on the east
coast of Sweden, illustrating the structure of magnetic iron-ores and
associated rocks and minerals, as well as the relation of granitic veins
to these ores, presented by Hilary Bauerman, Esq., F.G.S. 2nd.
A series of Devonian Plants from Gaspé, Lower Canada, presented
by Principal J. W. Dawson, LL.D., F.G.S. 3rd. A collection of
Jurassic Fossils, chiefly Brachiopoda, from Normandy, including a
series of minute fossils from the Lepteena-beds, presented by Ralph
Tate, Esq., F.G.S. 4th. A collection of Metamorphic Rocks, exhi-
biting traces of organic remains, from the Alps, presented by Sign.
Crescenzo Montagna. And 5thly, a collection of Devonian Corals
from Poland, presented by Sir R. I. Murchison, Bart., K.C.B.,
F.G.S.

The chief additions made to the “ British Collection ” during the
year are: Ist a series of Rhomboidal Specimens of Clay-ironstone
and Iron-sandstone from the Collingwood Quarry, Kent, and the
Clanmullen Quarry, near Edenderry, King’s County, presented by
Sir J. F. W. Herschel, Bart., F.G.S., and Capt. T. Longworth Dames ;
and, 2ndly, specimens of siliceous casts of corals from the Carboni-
ferous Limestone of County Dublin, presented by H. B. Brady, Esq.,
E.G.S.

Satisfactory progress has been made since the last Anniversary in

ANNUAL REPORT. ca
the renaming of the specimens in the British and Foreign Collec-
tions ; though more work of this kind would have been done, but
for the encouraging fact that last year the collections were consulted
to a much greater extent than was formerly the case. ‘This is pro-
bably owing in some measure to the recent increase in the number of
the Fellows, but it is doubtless due in some degree to the more acces-
sible and increasingly useful state of the collections.

The Sharpe Collection of Corals, chiefly Palzeozoic, which origin-
ally occupied 18 drawers, has been thoroughly examined, the spe-
cimens named by Dr. Duncan, and placed upon tablets by Mr. Tate,
and the duplicates taken out. Owing to the economy of space thus
obtained the collection now occupies but 10 drawers.

The Committee recommend that the duplicates of these and other
British fossils should be offered to the Museum of Practical Geology.

The Zoological Catalogue of the whole of the Coral-collections is
now in hand, and will shortly be completed. The formation of type-
collections of fossils belonging to other classes of animals is in con-
templation, and the zoological collection of Echinodermata has been
commenced. Some additions have been made to the nucleus of the
collection of Polyzoa; but in this and in other type collections there
is a great want of specimens to illustrate certain types of structure.

Twelve drawers containing fragile fossils, such as those of the
Red Crag, have been fitted with glass, and the cleaning, remounting,
and naming of the specimens are in progress.

The Collection of Bordeaux Miocene Fossils, occupying 11 drawers, |
has been thoroughly examined and arranged, the specimens have
been placed upon tablets, and the duplicates removed; and the
drawers containing the collection have been fitted with glass.

The following table contains a summary of the work done in the
Museum during the past year, in naming and arranging collections
of fossils.

Drawers.
femelamtl J. vi.0. 25": 3. Meg res gue. 2
sc, Ae Gabe AS. Baths soya 2
sigh cece lars ania agen eee es Bee iL
Ee ear a ahs Inferior Oolite ...... 9
eepaVarta bee Siirasere mete fe en 3)
aarGeaIx. ... os. 2 Miaodenes 2 ee Oe: 1f
Normandy ..... ... Jurassic & Cretaceous 4
ee eee Ee Cretaceous Woe, . vs a
*Zoological Collection of Corals ............ 10
Zoological Collection of Echinoderms ...... 3
Piuuecellameous Cordis 2%... ov bee ew bh
47

In concluding their Report the Committee desire to express their
opinion that the especial thanks of the Society are due to Dr. Dun-
can for his energetic and well-sustained labours in the Museum

* Corals, named by Dr. Duncan.

ae : ANNIVERSARY MEETING.

during the last three years ; and to record their satisfaction with the
manner in which Mr, Tate has discharged his duties in the Museum
during the past year.

J. GWYN JEFFREYS.
THOS. WILTSHIRE.
Rk. ETHERIDGE.

The Library.

The chief additions made to the Library by purchase last year are
Coquand’s ‘ Géologie et Paléontologie de la Province de Constantine,’ —
Massalongo’s ‘Saggio Fotografico di alcuni animali e piante fossili
dell’ Agro Veronese,’ Etallon and Thurmann’s ‘ Lethza Bruntrutana,’
Stoppanr’s ‘ Petrifactions d’Esino,’ and Huxley and Hawkins’s ‘Atlas
of Comparative Osteology.’ Amongst the donations Dr. Hochstetter’s
Geology of New Zealand, the accompanping volume on the Paleon-
tology of the Islands, and the second volume of M. Barrande’s ‘ Sys-
teme Silurien de la Bohéme’ are more especially worthy of mention.

The Map-collection has received some very valuable additions, in-
cluding the large geological map of the country round Bristol, in 19
sheets, presented by the author, W. Sanders, Esq., F.R.S., F.G.8.; a
complete copy of the “‘ Geologische Karte der Rheinproyinz und der
Provinz Westfalen,” presented by Herr von Dechen, For. Mem. G.S.,
through Sir R. I. Murchison, Bart., K.C.B., F.G.S.; the “ Carte géo-
logique de l’Espagne et du Portugal, presented by the authors,
MM. de Verneuil, For. Mem. G.S., and C. Collomb; several sheets
of the Geological Survey-map of Great Britain and Ireland, presented
by the Director-General, Sir R. I. Murchison, Bart., K.C.B., F.G.S.,
and of the Ordnance Survey-map of Great Britain, on the 1-inch and
6-inch scales, presented by the Director-General, Col. Sir Henry
James, F,G.S., and some of the sheets of the Geological Survey-map
of the Netherlands, presented by His Excellency the Minister for
the Netherlands.

The Committee beg to recommend that a larger sum should be ex-
pended annually in the purchase of Geological books than has
hitherto been voted for that purpose. They find that last year not
more than about £25 was expended in the purchase of books, and
about £30 for binding.

The Committee suggest the appointment of a standing Library
Committee, to meet on the first meeting-day of the Society in every
alternate month.

The Assistant-Secretary reports that he has received much as-
sistance from Mr. Horace Woodward in doing the current work of
the Library, and in making Diagrams for the Evening-meetings.

J. GWYN JEFFREYS.
THOS. WILTSHIRE.
R. ETHERIDGE.

ANNUAL REPORT. : Vv

Comparative Statement of the Number of the Socrety at the close of
the years 1864 and 1865.

Dec. 31, 1864. Dec. 31, 1865.

Compounders .........>» HOG. ope aes 167
Contributing Fellows .... BLA tks ans 395
Non-contributing Fellows 2A Nati a 469

| 1001 1031
Honorary Members...... Ge pte J. 3
Foreign Members........ Z's Ade a ee 44
Foreign Correspondents .. oe Miia wen ee as 39
Personage of Royal Blood 1 rh pao ss, 0

1092 ity

General Statement explanatory of the Alteration in the Number of
Fellows, Honorary Members, sc. at the close of the years 1864 and
1865.

Number of Compounders, Contributing and Non-con-

tributing Fellows, December 31, 1864...... 1001

Add Fellows elected during former year and paid
cu LEE os BS Se eee oe

Deduct Compounders deceased ........... Sa
Contributing Fellows deceased ............
Non-contributing Fellows deceased ........
Contributing Fellows resigned ............
Contributing Fellows removed ............

| Hs O1 CO > OO

1031

Members, Foreign Members, and Foreign
Correspondents, December 31, 1865........

Number of Personages of Royal Blood, "to
Add Foreign Correspondent elected in 1865 ......

Deduct Personage of Royal Blood deceased .... 1
Foreign Members deceased .......... ~
Foreign Correspondent deceased ...... fe) 6

V1 ANNIVERSARY MEETING.

Dzcrasep Frttows.
Personage of Royal Blood (1).
His Majesty the King of the Belgians.

Compounders (8).
The Earl of Ilchester. F. W. Simms, Esq.
Samuel Cartwright, Esq. Dr. 8. P. Woodward.

Henry Christy, Esq. Sir J. W. Lubbock, Bart.
W. G. Prescott, Esq. Lovell Reeve, Esq.

Residents and other Contributing Fellows (6).

E. L. Richards, Esq. | TT. E. Blackwell, Esq.
Dr. H. Falconer. W. B. Mitchell, Esq.
J. Macdonnell, Ksq. | G. Ei. Roberts, Esq.

Non-contributing Fellows (3).
Lieut.-Col. T. E. Sampson. | Nicholas Wood, Esq.
T. Hutton, Esq. |
Foreign Members (A).
Dr. C. H. Pander. | M. C. von Oeynhausen.
Prof. K. von Raumer. | Dr. J. G. Forchhammer.
Foreign Correspondent (1).
Dr. Albert Oppel.

_. Fetrows Rustenen.
Residents and other Oontributiny Fellows (4).

Lord Dufferin. George Whitmore, Esq.
Dr. G. C. Wallich. B. de Courcy Nixon, Esq.

Non-contributing Fellow (1).
KK. H. Sheppard, Esq.

Frettows Rremovep.

Residents and other Contributing Fellows (4).
Rev. F. F. Statham. Mark Fryar, Esq.
H. T. James, Ksq. , Dr. J. Winter.

ANNUAL REPORT. Vil

The following Persons were elected Fellows dwring the year 1865.

January 11th.—George Elliott, Esq., 23 Great George Street, West-
minster, §.W.; Robert Hannah, Esq., 2 Alfred Place West, South
Kensington, 8. W.; Henry Robinson, Esq., Assoc. I.C.E., 2 Dela-
hay Street, ‘Westminster, S.W., and Carlton Hill, St. J ohn’s Wood,
N.W.; Robert P. Roupell, Esq., Q.C., 13 Park Lane, Hyde Park,
W.; Captain John Sackville Swann, H .M. 22nd Regt., Malta ; and
John Edmund Thomas, Esq., C.E., Rhayader.

25th.—William Grylls Adams, Esq., M.A., Lecturer on Natural

_ Philosophy in King’s College, London ; and Capt. Stewart Smyth
Windham, 14 Connaught Place, W.

February 8th.—Capt. William Arbuthnot, 25 Hyde Park Gardens,
W.; Robert Bell, Esq., Professor of Geolog gy in Queen’s College,
Canada West; William Henry Leighton, Esq., 2 Merton Place,
Chiswick ; and Viscount Milton, E.R.G.S., of Wentworth Park,
and 4 Grosvenor Square, W.

22nd.—C. Gainer, Esq., M.A., St. Mary’s Hall, Oxford; John
Wesley Judd, Esq., 2 Burngreave View, Sheffield; Francis R.
Spry, Esq., Ashford, near Hornsey; The Hon. Arthur Strutt, 88
Eaton Square, W.; and Samuel Long Waring, Hsq., The Oaks,
Norwood. |

March 8th.—The Rey. T. H. Browne, High Wycombe, Berks; Thomas
Grange Hurst, Esq., Mining Engineer, Backworth, Northumber-
land; and W. R. Willams, Esq., Mining Engineer, Dolgelly,
North Wales.

22nd.—Henry Turner, Esq., Mottingham, Kent.

April 5th.—Henry Clark Barlow, M.D., Newington Butts, 8.E. ;
Townshend Monckton Hall, Esq., Pilton Parsonage, near Barn-
staple; John Lawson, Esq., C.E., 34 Parliament Street, S.W. ;
William Milnes, Esq., Blackheath, Kent, and Yeolm Bridge, South
Devon; J. Samuel Perkes, Esq., C.E., Belvedere House, West
Dulwich, 8.; and Minos Claiborne Vincent, Esq., C.E., Frankfort,
Ohio, U.S.

20th.—J. W. Conrad Cox, Esq., B.A., 4 Grove Hill, Wood-
ford, N.E., and 32 Westbourne Place, Eaton Square, W.; Henry
K. Jordan, Esq., Tenby House, Cotham, Bristol; and Thomas J.
Sells, Esq., M. R.C. S: Guildford, Sunreyau

May 10th.— Absalom Bennett, Esq. ., Marazion, Cornwall; Joseph
Brown, Esq., Q.C., of the Middle Temple, 54 Avenue Road,
Regent’s Park, N.W.; The Rev. John Magens Mello, M.A., In-
cumbent of St. Thomas’s Brampton, Chesterfield; and George
Noakes, Esq., 3 Grosvenor Villas, St. Bartholomew Row, Hollo-
way, N.

—— 24th.—James Philip Baker, Esq., Wolverhampton; George
William Cline, Esq., 38 Albermarle Street, Piccadilly, W.; James
Coutts Crawford, Esq., Wellington, New Zealand; Theodore H.
Hughes, Esq., of the eal Survey of india and Charles
Ottley Groom Napier, Esq., Bristol.

June 21st.—Samuel Bailey, Esq., Mining Engineer, The Pleck,

Vill ANNIVERSARY MEETING.

Walsall; William Keene, Esq., Sydney, New South Wales; and
the Rey. Benjamin Waugh, Newbury, Berks.

November 8th.—Thomas cy allven Danby, Esq., B.A., Downing Col-
lege, Cambridge; William Poole King, Esq., Avon Side House,
Clifton, Bristol; James L. Lobley, Esq., 50 Lansdowne Road,
Kensington Park, 8.W.; John Richardson, Esq., C.E.; James
Clifton Ward, Esq., Clapham Common; and Samuel Hansard
Yockney, Esq., M.1.C.E.

22nd.—Robert Lightbody, Esq., Ludlow, Salop.

December 6th.—W. Phipson Beale, Esq., 27 Victoria Street, S.W. ;
Henry Braddon, Esq., 5 Dane’s Inn, Strand, W.C.; Captain Robert
Clipperton, H.B.M. Consul at Kertch; Tellef Dahll, Esq., Kra-
gere, Norway; R. A. Eskrigge, Esq., 24 The Albany, Old Hall
Street, Liverpool; Hugh Frederick Hall, Esq., Liverpool ; Hed-
worth Hylton Jolliffe, Esq., Merstham, Surrey; Edward Myers,
Esq., 29 Summer Hill Terrace, Birmingham ; George Pycroft, Esq.,
M.R.C.S.E., Kenton, Exeter; Ferdinand Stoliczka, Ph.D., of the
Geological Survey of India, Caleutta; Erwin Harvey Wadge, Esq.,
Stradbrook Hall, Blackrock, Co. Dublin, Ireland; Henry Augustus
Ward, Esq., Professor of Natural Sciences in the University of
Rochester, New York; and Frederick Williams, Esq., M.P.,
Goonvrae, near Truro.

—— 20th.—Hugh Leonard, Esq., C.E., Calcutta; Wilham Lyon,
Ksq., J.P., Wellington, New Zealand ; Moses Pullen, Esq., Pains-
wick, Gloucestershire ; and Charles Stavely Rooke, Esq., M.1.C.E.,
12 Bleinham Terrace, Leeds.

The following Person was elected a Foreign Correspondent during the
year 1865.

March 8th.—Prof. C. Nilsson, of Stockholm.

The following Donations to the Musnum have been received since
the last Anniversary.

British Speewmens,

Two Fossil Plants from the Coal-measures of Dudley ; presen by
H. Beckett, Esq., F.G.S.

Rhomboidal specimens of Clay Ironstone and Iron- sandstone from
the Collingwood and Clanmullen Quarries; presented by Sir
J. F. W. emenen Bart., F.R.S., F.G.8., and Capt. T. Longworth
Dames.

Twelve specimens of Lead and Copper from various localities ; pre-
sented by J. W. B. Owen, Esq., M.A.

Siliceous Casts of Corals from the Carboniferous Limestone near
Dublin; presented by H. B. Brady, Esq., F.G.S.

Foreign Specimens.

Rock-specimens from Peru ; presented by R. Spruce, Esq.

ANNUAL REPORT. 1x

Cast of Ovibos moschatus, Blainv.; presented by M. E. Lartét, For.
Mem. G.S.

A Collection of Rocks and Minerals from Roslagen, Sweden ; pre-
sented by H. Bauerman, Ksq., F.G.S.

Fourteen specimens of Devonian Plants from Gaspé ; presented by
Dr. J. W. Dawson, F.R.S8., F.G.S.

Five specimens of Cannel Coal from New South Wales; presented
by the Rev. W. B. Clarke, M.A., F.G.S.

Devonian Corals from Poland; presented by Sir R. I. Murchison,
Bart... FIR.S:, F.G.8.

Jurassic Fossils from Normandy; presented by RalphTate, Esq., F.G.S.

Tertiary Echinoderms from Trinidad; presented by R. J. L. Guppy,
Kisq.

Mars, CHARTS, ETC., PRESENTED.

Carte Géologique de l’Espagne et du Portugal, par MM. E. de Ver-
neuil et E. Collomb. 1849 a 1862; presented by the authors.

Karten und Mittheilungen des Mittelrheinischen Geologischen Ve-
reins. Section Darmstadt, von R. Ludwig, 1864; presented by
the author.

_ Geological Survey of Victoria. Sheets 3 and 15; presented by A.
R. C. Selwyn, Esq.

Mapa geologico de la Provincia de Madrid, por Don Casiano de Prado,
For. Mem. G.S.; presented by the author.

Map of the Bristol Coal-fields and country adjacent, in 19 sheets,
geologically surveyed by William Sanders, F.G.S.; presented by
the author.

The Chain of Mont Blanc, from an actual survey in 1863-64, by A.
Adams-Reilly, A.C., F.R.G.S. 1865; presented by the author.
Geological Map of Scotland, by Sir R. I. Murchison and A. Geikie ;

presented by Sir R. I. Murchison, Bart., K.C.B., F.R.S., F.G.S.
Geological Sketch-Map and sections of the Province of Wellington,
New Zealand, by J. Coutts Crawford, F.G.S.; presented by the
Geological Survey of New Zealand.

Geologische Karte der Rheinprovinz und der Provinz Westfalen, by
Dr. H. von Dechen; presented by Sir R. I. Murchison, Bart.,
meh LORS. F.GS.

Geologische Karte der Provinz Victoria, by A. R. C. Selwyn; pre-
sented by Dr. A. Petermann.

Geological Survey of Great Britainand Ireland. England. Nos.4,6,
(a 9, 45 (N.E. &8.E.), 46 (N.W. & S.W.), 52, 81 ‘(N.W. & S.W.),
and 89 (S.E.).—Scotland. Nos.33,34, and41.—Ireland. Nos. 99,
114-117, 118, 122-127, and 133- 135.—England. Section No.
65.—Ireland. Explanations of Sheets Nos. 102, 112, 144, 146,
147, 153, 157, and 163-175.

Sveriges seologiska Undersokning. Nos. 6 to 13. 1863-64; pre-
sented by Dr. A. Erdmann.

Seventy-five Miscellaneous Charts, published by the Dépot de la —
Marine ; presented by the Dépét de la Marine.

x ANNIVERSARY MEETING.

Ordnance Survey of Great Britain. Maps, 6-inch scale :—North-
umberland, Sheets 15, 72, 73, 79-82, 85-87, 91-95, 100-103,
106, 106a & 6-108, 110, 111. Stirlingshire, Sheets, 8, 20-26,
28-30, 32, 33, 35, 36. Dumbartonshire, Sheets 2-4, 6-14, 16—
18, 23, 26. Roxburgshire, Index-sheet. Lanarkshire, Sheet 6.
Forfarshire, Sheets 1—7, 9-18, 22, 23, 40, 41, 438-46, 48-55.—
Ordnance Survey of England. 1-inch scale :—Sheets 98, 99, 105,
110.—Ordnance Survey of Ireland. 1-inch scale :—Sheets 7, 8,
14,135 °37,,90, 121.

Geological Survey Maps of Holland. Sheets 3, 4,8, 11, 17; pre-
sented by His Excellency the Minister for the Netherlands.

Geologisk kart over Christiana Omegn, af Theodor Kjerulf. 1864;
presented by the Royal University of Christiana.

Carte Agronomique des environs de Paris, par M. Delesse ; presented
by the author.

- 4

Four Photographs of Fossils from Queensland and New South Wales ;
presented by W. Keene, Esq., F.G.S.

Photograph of Teler rpeton Elginense; presented by the ie G. H.
Roberts, Esq., F.G.S.

Diagram showing the mode of construction of the Scismenneen by
Ticueecar C. Ramstedt ; presented by the author.

The following Lists contain the Names of the Persons and Public
Bodies from whom Donations to the Library and Museum have been
received since the last Anniversary, February 17, 1865.

I. List of Societies and Public Bodies from whom the Society has
received Donations of Books since the last Anniversary Meeting.

Abbeville, Imperial Society of | Caen. Linnean Society of Nor-
Emulation of. mandy.
Calcutta. Geological Survey of
Basel, Natural History Society India.

of.

Belgium, Geological Survey of.

Berlin. German Geological So-
ciety.

Berwick. Natural History Field-
club.

Bombay, Geographical Society of.

Boston, Museum of Comparative
Zoology of.

, Natural History Society

of.

Breslau. Silesian Society for
Fatherland Culture.

Brussels. Royal Academy of
Sciences of Belgium.

, Bengal Asiatic Society at.

Cambridge (Mass). American
Philosophical Society.

. American Academy
of Arts and Sciences.

Cherbourg, Society of Natural
Sciences of.

Christiana, Royal University of.

Darmstadt. Geological Society
of the Middle Rhine.

Dijon, Academy of Natural Sci-
ences of.

Dublin. Geological Survey of
Ireland.

—_——

ANNUAL REPORT. x

Dublin. Royal Irish Academy.
Royal Society.

Royal Geological Society
of Ireland.

Edinburgh, Geological Society of.
, Royal Society of.
Exeter. Devonshire Association.

France, Acclimatization Societyof.
, Geological Society of.

Geneva, Physical and Natural
History Society of.
Glasgow, Geological Society of.

Heidelberg, Natural History So-
ciety of.

Lausanne. Vaudoise Society of
Natural Sciences.

Leeds, Philosophical and Literary
Society of.

Liverpool, Geological Society of.

Lancashire and Cheshire

Historic Society.

, Philosophical Society of.

London, Anthropological Society
of.

, Art Union of.

British Association.
——, Chemical Society of.
Geological Survey of
Great Britain.

Geologists’ Association.
Institute of Actuaries of
Great Britain and Ireland.
Institute of Civil Engi-
neers.

, Linnean Society of.

——. Mendicity Society of.
——, Microscopical Society of.
——. Palzontographical Society.
——, Photographic Society of.
Ray Society.

Royal Asiatic Society of
Great Britain.

, Royal Astronomical So-
ciety of.

ee
e

London, Royal College of.

, Royal Geographical So-

ciety of.

, Royal Horticultural So-

ciety of.

. Royal Institution of Great

Britain.

, Royal Society of.
Secretary of State for

War.
, Zoological Society of.
Lyons, Imperial Academy of
Sciences of.

Madrid, Academy of Sciences of.

Manchester, Geological Society
of.

Melbourne, Public Library of.

Royal Society of Victoria.

Milan, Society of Natural Sciences
of.

Montreal, Natural History So-
ciety of.

Moscow, Imperial Academy of
Naturalists in.

Munich, Academy of Sciences of.

Neuchatel, Society of Natural
Sciences of.
Nova Scotian Institute.

Padua, Royal Academy of Sci-
ences of.

Palermo, Institute of Natural
Sciences of.

Paris. Academy of Sciences.
——. Dépdt Général de la Ma-
rine.

School of Mines.

——. Institute of the Provinces.

Philadelphia. Academy of Na-
tural Sciences.

American Philosophical
Society.

Plymouth Institution.

Presburg, Natural History So-
ciety of.

St. Petersburg, Imperial Academy
of.

xii ANNIVERSARY MEETING.

Shanghai. North China branch
of the Royal Asiatic Society.
Southampton. Ordnance Survey.
Stockholm. Royal Swedish Aca-

demy.

Tasmania, Royal Society of.

Teign Naturalists’ Field-club.

Toronto. Canadian Institute.

Turin. Alpine Club.

——. Royal Institute of Lom-
bardy.

Vienna, Geological Institute of.
, Imperial Academy of.

Warwickshire Naturalists’ Field-
club.

Washington. Patent Office.

. Smithsonian Institution.

Wurtemburg, Natural History

Society of.

Yorkshire (West Riding). Geo-
logical and Polytechnic So-
ciety.

II. List containing the names of the Persons from whom Donations
to the Library and Museum have been received since the last

Anniversary.

Adams-Reilly, A., Esq.

Ansted, Prof. D. T., F.G.S.

American Journal of Science and
Arts, Editor of the.

Archiac, Vicomte A. d’, For.Mem.
G.S.

Atheneum, Editor of the.

Bagot, A. H., Esq.

Barrande, M. J., For.Mem.G.S.

Bauerman, H., Esq., F.G.S.

Beckett, H., Esq., F.G.S.

Benecke, M. E. W.

Bianconi, Prof. G.

Binney, E. W., Esq., F.G.S.

Bischof, Prof. G., For.Mem.G.8.

Blanford, H. F., Esq., F.G.S.

Boucher de Pemhes, M. » Hor. Corr.
G.S.

Boult, J., Esq.

Brady, H.B., Esq., F.G.S.

Brown, R., Esq.

Campbell, J. F., Esq.

Carter, Dr. H. J.

Catullo, Sign.

Charnock, Dr. R. 8.

Christy, the Executors of the late
H., Esq., F.G.S.

Clarke, Rev. W. B., F.G.S.

Codrington, T. Esq., F.G.S.

Colliery Guardian, Editor of the.
Collomb, M. E.
Crawford, J. C., Esq., F.G.S.

Dames, Capt. T. L.

Dawkins, W. B., Esq., F.G.S.

Dawson, Dr. J. W., F.G.S.

Delesse, Prof. A., For.Mem.G.8.

Deshayes, Prof. G. P., For.Mem.
G.S.

Duncan, Dr. P. M., Sec.G.S.

Edwards, Dr. H. Milne- For.
Mem.G.8.

Egerton, Sir P. de M. G., Bart.

FiGes:
Erdmann, Dr. A.

Favre, M. A.

Fonvielle, M. de.

Foote, R. B., Esq.

Forchhammer, the late Prof. G.,
For.Mem.G.8.

Fuhlrott, Prof. C.

Garrigou, M. F.

Gastaldi, Sign. B., For.Corr.G.8. -

Geinitz, Dr. H. B., For.Mem.G.S8.

Goeppert, Dr. H. R., For.Mem. |
G.S

Groot, M. C. de.

ANNUAI REPORT.

Guilbert, M. L.
Gumbel, Herr Bergm., For.Corr.
G.S

Pian, Rey. J., F.G.8.
' Guppy, R. J. L., Esq.
Gutzeit, T. von.

iaast, Dr. J., F.GS8.

Haswell, G. C., Esq.

Hauer, F. R. von., For.Corr.G.S.

Hébert, Prof. E., For.Corr.G.S.

Heer, Dr. O., For.Corr.G.S.

Helmersen, Gen. G. von, For.
Mem.G.8.

Herschel, Sir J. F. W., F.G.S.

ind. Prot. H. Y.

Hochstetter, Dr. F.

Hon, M. H. Le.

Hull, E., Esq., F.G.S.

Intellectual Observer, Editor of
the.

James, Col. Sir H., F.G.S.
Jervis, W. P., Esq., F.G.S.
Jones, Prof. T. R., F.G.S.
Jordan, H. K., Esq., F.G.S.

- Journal of the Society of Arts,
Editor of the.

‘Karrer, Dr. F.

iReene, W., Ksq., F.G.S.

King, Prof. W.

Kirkby, J. W., Esq.

Keenen, Baron von.

Kokscharow, M. N. von.

Koninck, Prof. L. de, For.Mem.
G.S.

Lankester, E. R., Esq.
Lartét, M. E. , For. Mem.G.8.
Lartét, M. Ee

Laube, Dr. G. C.

Laugel, M. A., F.G.S.
Lavizzari, Dr. L.

-Lentillac, M. de.

Liebig, Baron J. von.
Locke, J., Esq.

Logan, Sir W. E., F.G.S.
London Review, Editor of the.

xii

Longman and Co., Messrs.
Luca, Sign. S. de.

Ludwig, M. R.

Lyell, Sir Charles, Bart., F.G.S.

Mackie, 8. J. Esq., F.G. s

Marés, Dr, ice

Marmora, Gen. A. della.

Martin, M. J.«

Martins, Dr. C., For.Corr.G.S.

Maw, G., Esq., F.G.S.

Mining and Smelting Magazine,
Editor of the.

Montagna, M. C.

Mortillet, M. G. de.

Murchison, Sir R.I., Bart., F.G.S.

Nigeli, Dr. C.

Omboni, Sign. G.
Oppel, the late Dr. A., For.Corr.
G.S

Owen, J. W. B., Esq.

Page, D., Esq., F.G.S.

Parker, W. K., Esq.

Perrey, M. A.

Petermann, Dr. A.

Phillips, Prof. J., F.G.S.
Ponzi, Sign. G.

Prado, Sign. C.de, For. Mem.G.S.

Quetelet, M. A.

Ramstedt, Lieut.-Col. C.

Reader, Editor of the.

Renevier, M. E.

Reuss, Dr. A. E., For.Corr.G.S.

Roberts, the late G. E., Esq.,
iE Gapa

Romanofski, M. G.

Sanders, W., Esq., F.G.S.

Seeley, H. Esq., F:G.S8.

Selwyn, A. R. C., Esq.

Sismonda, Prof. A., For.Mem.
GS

Soulby, T., Esq.

South, Sir J.

Spratt, Capt. T. A. B., F.G.S.

X1V ANNIVERSARY MEETING.

Spruce, R. Esq. Tylor, E. B., Esq.
Stoliczka, Dr. F., F.G.S. Verneuil, M. E. de, For. Mem.
Studer, Prof. B., For. Mem. G.S. G.S.
Suess, Prof. E., For.Corr.G.S. ;
Waagen, Dr. W.

Tate, G. Hsq., F.G.8. Watelet, M. A.

Tate, R. Esq., F.G.S. Whitaker, W., Esq., F.G.S.
Tawny, E. B., Esq., F.G.S. Winchell, Prof. A.

Tennant, Prof. J.,:F.G.S. Winkler, Dr. T. C.

Theobald, Prof. Winslow, Dr. C. F.

Tribner and Co., Messrs. Wood, Rev. HU He aeGass
Tylor, Au; Esq) :G:s: Wood, S. V., jun., Esq., F.G.S.

Inst of Pavers read since the last Anniversary Meeting,
February 17th, 1865.

1865.

February 22nd.—On the Lower Silurian Rocks of the South-east
of Cumberland and the North-east of Westmoreland, by Prof. R.
Harkness, F.R.S., F.G.S.

_____._"_ Note on the Volcanic Tufa of Latacunga, at the foot
of Cotopaxi; and on the Cangaua, or Volcanic Mud a the Quite-
nian Andes, by R. Spruce, Esq.; communicated by Sir R. I.
Murchison, Bart., K.C.B., F.R.S., F.G.S.

On the Discovery of Flint Implements in the Drift
at Milford Hull, Salisbury, by Dr. H. P. Blackmore; communi-
cated by J. Evans, Esq., F.R.S., F.G.S.

March 8th.—A Description of the Echinodermata from the Strata on
the South-east Coast of Arabia, and at Bagh on the Nerbudda, in
the Collection of the Geological Society, by P. Martin Duncan,
M.B., Sec.G.S.

On the Fossil Contents of the Genista Cave, Gibraltar,
by G. Busk, Esq., F.R.S., F.G.8., and the late Hugh Falconer,
M_D., ERS EGS:

March 22nd.—Notes on the Caves of Gibralter, by Lieut. C. Warren,
R.E.; communicated by Sir R. I. Murchison, Bart., K.C.B., F.R.8.,
ReGeS: |

On the asserted Occurrence of Human Bones in the
ancient Fluviatile Deposits of the Nile and the Ganges, with com-
parative Remarks on the Alluvial Formation of the two Valleys, by
the late Hugh Falconer, M.D., F.R.S., F.G.S.

April 5th.—On some Tertiary Deposits in the Colony of Victoria,
Australia, by the Rev. J. E. T. Woods, F.L.8., F.G.8.; with a
Note on the Corals, by P. M. Duncan, M.B., Sec.G.S.

ee On the Chalk of the Isle of Thanet, by W.. Whitaker,
HequvB A. WE GES:

——_——— On the Chalk of Buckinghamshire, and on the Tot-

ternhoe Stone, by W. Whitaker, Esq., B.A., F.G.S.

——— On the Chalk of the Isle of Wight, by W. Whitaker,

Esq., B.A., F.G.S.

ANNUAL REPORT. XV

1865. ;

April 26th.—On the Character of the Cephalopodous Fauna of the
South-Indian Cretaceous Rocks, by Dr. Stoliczka, Ph.D.; com-
municated by the Assistant-Secretary.

———- On the Growth of Flos Ferri, or Coralloidal Arragonite,
by W. Wallace, Esq.; communicated by W. W. Smyth, Ksq.,
Hoe. E.G.S:

—_—_ —_ Notes accompanying some Rhomboidal Specimens of

Tron-Sandstone, &c., presented to the Society, by Sir J. F. W. Her-
schel, Bart., K.C.H., F.R.S., F.G.S.; with a Note, by Capt. T. L.
Dames ; communicated by Sir C. Lyell, Bart., F.R.S., F.G.S.

May 10th.—On the Azoic and Paleozoic Rocks of Southern New
Brunswick, by G. F. Matthew, Esq.; communicated by J. W.
Dawson, LL.D., F.R.S., F.G.8.

—_—______— Results of Geological Observations in Baden and
Franconia, by Dr. F. Sandberger, For.Corr.G.8.

————— On the Changes rendered necessary in the Geological
Map of South Africa by recent Discoveries of Fossils, by R. N.
Rubridge, M.B., F.G.S.

May 24th.—Additional Observations on the Raised Beach of San-
gatte with reference to the Date of the English Channel, and the
presence of Loess in the Cliff Section, by J. Prestwich, Esq., F.R.S.,
Treas.G.8,

On the Superficial Deposits of the Valley of the Med-
way, with remarks on the Denudation of the Weald, by C. Le N.
Foster, D.Sc., F.G.S., and W. Topley, Esq., F.G.8.

June 7th.—Note on Ovibos moschatus, Blainville, by M. E. Lartét,
For.Mem.G.8.

On some Additional Fossils from the Lingula-fiags,

by J. W. Salter, Esq., F.G.S.; with a Note on the Genus Anopo-

lenus, by H. Hicks, Esq., F.G.S.

——— On some New Species of Crustacea belonging to the

Order Eurypterida, by Henry Woodward, Esq., F.G.8., F.Z.8.

On the Discovery of a New Genus of Cirripedia in
the Wenlock Limestone and Shale of Dudley, by Henry Wood-
ward, Ksq., F.G.S., F.Z.S.

———_—— On a New Genus of EHurypterida from the Lower
Ludlow Rock of Leintwardine, Shropshire, by Henry Woodward,
Msg. FG.S., F.Z.8.

June 21st.—On the Carboniferous Rocks of the Valley of Kashmere,
by Capt. H. Godwin-Austen; with Notes on the Carboniferous
Brachiopoda, by T. Davidson, Esq., F.R.S., F.G.S.; and an In-
troduction and Résumé, by R. A. C. Godwin-Austen, F.R.S., For.
Mem.G.8.; communicated by R. A. C. Godwin-Austen, Esq.,
PORS,, &e,

On the Mammalian Remains found by E. Wood, Esq.,
near Richmond, Yorkshire, by W. B. Dawkins, Esq., M.A., F.G.S. ;
with an Introductory Note on the Deposit in which they were
found, by E. Wood, Esq., F.G.8., and .G. E. Roberts, Esq.,
IG.S. .

XV1 ; ANNIVERSARY MEETING.

1865.

November 8th.—On the Sabnienes Forest-beds in Porlock Bay, by
R. A. C. Godwin-Austen, Esq., F.R.S., For.Sec.G.8. —

On the Marine Origin of the ‘ Parallel Roads’ of
Glen Roy, by the Rev. R. Boog vaon: BFA Se EGss:

November 22nd.—On Impressions of Selenite in the Woolwich Beds
and London Clay, by P. Martin Duncan, M.B., Sec.G.S.

—_—— On the Relation of the Chillesford Beds to the Norwich

Crag, by the Rev. O. Fisher, M.A., F.G.S.

December 6th.—On the Western Limit of the Rhetic Beds in South
Wales, and on the position of the Sutton Stone, by E. B. Tawney,
Esq., F.G.S.; with a Note on the Corals of the Sutton Stone, by
P. Martin ine M.B., Sec.G.8.

Notes on a Section of the Lower Lias and Rheetic
Beds near Wells, Somerset, by the Rev. P. B. Brodie, M.A., F.G.S. .

December 20th.—On the Conditions of the Depositions of Coal, by
J. W. Dawson, LL.D., F.RBS., F.G.S.

1866.

January 10th.—On the Origin and Microscopic Structure of the so-
called Kozodn-Serpentine, by Prof. W. King and Dr. T. H. Row- —
ney; communicated by Sir R. I. Murchison, Bart., F.R.S., F.G.S.

Supplemental Notes on the Structure and Affinities
of Hozoon Canadense, by W. B. Carpenter, M.D., F.R.S., F.G.S.

January 24th.—Notes on Belgian Geology, by R. A. C. Godwin-
Austen, Esq., F.R.S., For.Sec.G.8.

February 7th.—On the Mode of Formation of certain Lake-basins
in New Zealand, by W. T. Locke Travers, Esq.; communicated
by Sir C. Lyell, Bart., D.C.L., F.RB.S., E.G.S.

On the Occurrence of Dead ‘Littoral Shells in the Bed

of the German Ocean, forty miles from the coast of Aberdeen, by

Robert Dawson, Esq, ; communicated by T. F. Jamieson, Esq.,

F.G.S.

On the Glacial Phenomena of Caithness, by T. F.
Jamieson, Esq., F.G.8.

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 resolved,—

1. That the thanks of the Society be given to W. J. Hamilton,
Esq., retiring from the office of President.

2. That the thanks of the Society be given to Dr. Meryon, J.
Carrick Moore, Esq., and Sir R. I. Murchison, retiring from the
offices of Vice-Presidents.

3. That the thanks of the Society be given to Warington W. .
Smyth, Esq., retiring from the Office of Secretary.

4, That the thanks of the Society be given to Robert Chambers,
Esq., the Rev. Robert Everest, Sir John Lubbock, and Dr. Meryon,
retiring from the Council.

ANNUAL REPORT.

XVil

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 :—

OFFICERS.

PRESIDENT.
Warington W. Smyth, Esq., M.A., F.R.S.

VICE-PRESIDENTS.

Sir P. de M. G. Egerton, Bart., M.P., F.R.S.

Professor T. H. Huxley, F.R.S. & LS.
Sir Charles Lyell, Bart., D.C.L., F.R.S.

Professor A. C. Ramsay, F.R.S.

SECRETARIES. -

P. Martin Duncan, M.B.
Johu Evans, Esq., F.R.S., F.S.A.

FOREIGN SECRETARY.
R. A. C. Godwin-Austen, Esq., F.R.S.

TREASURER.

Joseph Prestwich, Esq., F.R.S.

H. W. Bristow, Esq., F.R.S.

COUNCIL.

P. Martin Duncan, M.B. wa eles y

Sir P. de M. G. Egerton, Bart.,
mae. FR.

Earlof Enniskillen, D.C.L.,F.R.S. 1 I NSE

_ Robert Etheridge, Esq., F.R.S.E.

John Evans, Esq., F.R.S., F.S.A.

R. A. C. Godwin- Austen, Kisq. 5
E.R.S.

Professor T, H. Huxley, F.R.S.
& LS.

Professor John Moris.
Sir R. I. Murchison, Bart., K.C.B.,

John Carrick Moore, Esq., M.A.,

Robert W. Mylne, Esq., F.R.S.
Joseph Prestwich, Esq., F.R.S.
Professor A. C. Ramsay, F.R.S.

Warington W.Smyth, Esq.,M.A.,
W. J. Hamilton, Esq., F.R.S. RRS.

Capt. T. A. B. Spratt, R.N., C.B.,
PRIS:

J. Gwyn Jeffreys, Esq., F.R.S. Lieut.-Col. R. Strachey, R.E.,
Professor T. Rupert Jones. F.R.S. & LS.

M. Auguste Laugel.

Sir Charles liyell, Bart., D.C. L., F.R.A.S.

F.R.S.
VO. XXUL,

Rev. Thomas Wiltshire, M.A.,

XVill
LIST OF

THE FOREIGN MEMBERS

OF THE GEOLOGICAL SOCIETY OF LONDON, 1 1866.

Date of
Hlection.

1818. Professor G. C. Gmelin, Tiibingen.

1819. Count A. Breuner, Vienna.

1819. Signor Alberto Parolini, Bassano.

1822. Count Vitaliano Borromeo, Milan.

1823. Professor Nils de Nordenskiold, Helsingfors.

1827. Dr. H. von Dechen, Bonn.

1828. M. Léonce Elie de Beaumont, Sec. Perpétuel de l’Instit. France,
For. Mem. R.S., Paris.

1829. Dr. Ami Boué, Vienna.

1829. J.J. d’Omalius d’Halloy, Halloy, Belgium.

1889. Dr. Ch. G. Ehrenberg, For. Mem. R.8., Berlin.

1840. Professor Adolphe T. Brongniart, For. Mem. R.S., Pars.

1840. Professor Gustav Rose, Berlin.

1841. Dr. Louis Agassiz, For. Mem. R.S., Cambridge, Massachusetts.

1841. Professor G. P. Deshayes, Paris.

1844, William Burton Rogers, Esq., Boston, U.S.

1844, M. Edouard de Verneuil, For. Mem. R.S., Paris.

1847. M. le Vicomte B. d’Archiac, Paris.

1848. James Hall, Esq., Albany, State of New York.

1850. Professor Bernard Studer, Berne.

1850. Herr Hermann von Meyer, Frankfort-on-Maine.

1851. Professor James D. Dana, New Haven, Connecticut.

1851. General G. von Helmersen, S¢. Petersburg.

1851. Hofrath W.-K. Haidinger, For. Mem. R.S., Vienna.

1851. Professor Angelo Sismonda, Zuri.

1853. Count Alexander von Keyserling, Dorpat.

1858. Professor L. G. de Koninck, Lnége.

1854, M. Joachim Barrande, Prague.

1854, Professor Karl Friedrich Naumann, Lezpsie.

1856. Professor Robert W. Bunsen, For. Mem. R.S., Hezdelberg.

1857. Professor H. R. Goeppert, Breslau.

1857. M. K. Lartét, Paris.

1857. Professor H. B. Geinitz, Dresden.

1857. Dr. Hermann Abich, Tiflis, Northern Persia.

1858. Dr. J. A. E. Deslongchamps, Caen.

1858. Herr Arn. Escher von der Linth, Zerich.

1859. Professor A. Delesse, Paris.

1859. Dr. Ferdinand Roemer, Breslau.

1860. Dr. H. Milne-Edwards, For. Mem. R.S., Paris.

xix

1861. Professor Gustav Bischof, Bonn.

1862. Senor Casiano di Prado, Madrid.

1862. Baron Sartorius von Waltershausen, Géttingen.
1862. Professor Pierre Merian, Basle.

1864, Professor Paolo Savi, Pisa.

1865. M. Jules Desnoyers, Paris.

LIST OF
THE FOREIGN CORRESPONDENTS

OF THE GEOLOGICAL SOCIETY OF LONDON, 1 1866.

Election.

1863. Professor Beyrich, Berlin.

1863. M. Boucher de Perthes, Adbeville.
1863. Herr Bergmeister Credner, Gotha.
1863. Professor Daubrée, Paris.

1863. M. Desor, Neuchiitel.

1863. Professor Favre, Geneva.

1863. Signor Gastaldi, Zuri.

1863. Dr. C. T. Gaudin, Lausanne.

1863. M. Paul Gervais, Montpellier.

1863. Herr Bergmeister Gumbel, Munich.
1863. Franz Ritter von Hauer, Vienna.
1863. Professor E. Hébert, The Sorbonne, Paris.
1863. Rev. Dr. O. Heer, Zurich.

1863. Dr. Moritz Hornes, Vienna.

1863. Dr. G. F. Jager, Stuttgart.

1863. Dr. Kaup, Darmstadt.

1863. Dr. Theodor Kjerulf, Christeana.
1863. M. von Kokscharow, St. Petersburg.
1863. Dr. Leidy, Philadelphia.

1863. M. Lovén, Stockholm.

1863. Lieut.-Gen. Count Alberto Ferrero della Marmora, Turin
1863. Count A. G. Marschall, Vienna.

1863. Professor G. Meneghini, Pisa.

1863. M. Morlot, Berne.

1863. M. Henri Nyst, Brussels.

1863. Il Marchese Lorenzo Damaso Pareto, Genoa,

1863. Professor Pictet, Geneva.

1863. Signor Ponzi, Rome.

1863. Professor Quenstedt, Tubingen.

1863. Professor F. Sandberger, Bavaria.

1863. Signor Q. Sella, Zuri.
b2

1863. Dr. F. Senft, Hisenach.

1863. Dr. B. Shumard, St. Louis, Missourz.
1863. Dr. Steenstriip, Copenhagen.

1863. Prof. E. Suess, Vienna.

1863. Marquis de Vibraye, Paris.

1864. M. J. Bosquet, Maestricht.

1864. Dr. Charles Martins, Montpellier.
1865. Dr. C. Nilsson, Stockholm.

AWARDS OF THE WOLLASTON-MEDAL

UNDER THE CONDITIONS OF THE “ DONATION-FUND ”

ESTABLISHED BY

WILLIAM HYDE WOLLASTON, M.D., F.RS., F.GS., &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. 1851. The Rev. Prof. A.Sedgwick. -
1835. Dr. G. A. Mantell. 1852. Dr. W. H. Fitton.
1836. M. L. Agassiz. 1853. Cn er
1837. { Capt. P. T. Cautley. M. E. de Verneuil.
\ Dr. H. Falconer. 1854. Dr. Richard Griffith.

1838. Professor R. Owen. 1855. Sir H. T. De la Beche.
1839. Professor C. G. Ehrenberg. | 1856. Sir W. E. Logan.
1840. Professor A. H. Dumont. 1857. M. Joachim Barrande.
1841. M. Adolphe T. Brongniart. 1858, ue Hermann von Meyer.
1842. Baron L. von Buch. Mr. James Hall. :
1843. oi EK. de Beaumont. ; 1859. Mr. Charles Darwin.

M. P. A. Dufrénoy. 1860. Mr. Searles V. Wood.
1844, The Rev. W. D. Conybeare. |. 1861. Prof. Dr. H. G. Bronn.
1845. Professor John Phillips. 1862. Mr. Robert A. C. Godwin-
1846. Mr. William Lonsdale. Austen.
1847. Dr. Ami Boué. 1863. Prof. Gustav Bischof.

1848.-The Rev. Dr. W. Buckland. | 1864. Sir R. I. Murchison.
1849. Mr. Joseph Prestwich, jun. | 1865. Mr. Thomas Davidson.
1850. Mr. William Hopkins. 1866. Sir Charles Lyell.

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EstTiIMatsEs for
INCOME EXPECTED.

Due for Subscriptions on Quarterly Journal (con-

Sidered GGOd) Muarsavonssenstearcsnectcess sea ses'sse 80.0 0453
Due for Authors’ Corrections .......se.sscsecessscees 25 0
Due for Arrears (See Valuation-sheet) .........00. 450 0 O
555 O O

Ordinary Income.

From Resident Fellows, &c.; and Non-resi-

dentsiof 1859 tol@Gl! fvescseeceensooye woes TOO. OGNG
Admission-fees (supposed) Sette toe ei geanlaae 350
Compositions (Supposed) ........2..sseeeeeeeeee 300 0 O
————1350 0 O
Dividends’on’Consols” fetnccsccs-oessecenee sete caer os:sicetieeietsceieeeeme 140 0 O
Sale of Transactions, Proceedings, Library-cata-
logues, and Ormerod’s Index ............sserseeee 15 OV
Sale of Quarterly Journal ....00.....-0cs.c-ceacescnssen 140 0 0
Due from Longman and Co. in June oes.........00. 48 12 0
— 203 12 .0

Due from the Bequest-fund on account of monies expended

on Map, Library, and Museum <...0..2..teescan-ssckeceseusseer 238 14 11
Sale of Geological Map..........scsccsssosnceeess ood ence este aia 150) 0.

£2637 6 11

JOSEPH PRESTWICH, Treas.
Feb. 7, 1866.

the Year 1866.

EXPENDITURE ESTIMATED.

SiS One 8. ds
General Expenditure :

(ames and Insurance /..... 00.06. s sss ee evena 90P O10
FIGUSC-TEPAIFS “20 ce cece we cn ec cae tee e eens a 120 00
PMP MATE UMMM Meister ois ace, soakaip, aieieTe. nis, 52 8.0) «%0: mi eiore s)0 20 00
meee Parc ens(s wicce’ sscne’ «ae! joxe joie. ee'nie aie econ 35° 0" 0
MN ote iets 'otc fel crintuttto vate e eererecgce.ninie oth a's 30 0 0
Miscellaneous Printing, including Abstracts.... 25 0 0
Mieator Meetines.. 2... cae oe el ce es cerscree 20 0 0
Miscellaneous House-expenses ..........+--- 85 0 0
RPT RSE I wa ha abees latins (010) cinta a. 0/40; ¢ aha va yap eo 25 0 0
; 350 0 0
Salaries and Wages:
PASpattAMt- SECKELATY » = << «sec sc ccee ce snuiens se 200 0 0
Clerk and Accountant.............. Eee dsaay ete 90 0 0
Assistants in Museum and Library........ 2. se 14500
LCL iA bree olen SAAS ELAN OTS Aamo cetse 90° 0-0
PiMiseMmpId, 2... .5.0--< Spake ec nehe stall lexs cears 40 0 0
Occasional Attendance .....-ccccscrecccace 120 0
RERCELOE ako 5i6 nial So linw widnrave in awrapsiataatautiee 20 0 0
597 O O
NNN a cde sido aiiaes iesiansimevesecesouecese sae eas 150 00
ERE carton a tasrWak ss0\s as osidaee oom es Sed iadntaiwes duakansene 50 0 O
200 O O
Peerams at Mectings 2.0... ..scccccsesccccassaencnoees Sr 20210
Miscellaneous Scientific Expenditure ............... 40 0 O
45 |0' 0
Publications: Quarterly Journals ........... SER 550 O O
ns HEFAMSACHIONS: sicveacassesceseseoes Secnae (Reo On O
555; 0+. 0
i Geological Map ......... Hi caticde see eset dues 130°40) 70
Maem COMUeCCOT ANG Clerk ceccessascacsscccsensccescsenesstorecs aie 5OU1Siy 2
1927 18 2
Balance in favour of the Society ............0.. Suac iat nedaechors anos 19

£96876) hI

RECEIPTS.
££ ssd. eee:
Balance at Banker's January IF, 1865 ...........:.- 225 10 5
Balance in Clerk’s hands GUEGO, aie ls sce ape, epee LG. ie
Compositions) necelvedwer ier ste 22. cleo hie saree 389 O 6
Arrears of Adimissiomiees § y-a05 2 cee ccs oxen cues 79,12) 30
Arrears of Annual Subscription ............-+...9) aoa
Admisstonciees BUS6D Ie ore ees earn cece 2On, LOneO
Annual Contributions for 1865, viz.—
Resident Fellows ......... £552 6 O
Non-Resident Fellows ... 42 10 6
——a a | OA IG NG
Dividends.onConsols: 2:5. 5 tf gens cae os oe Se ee 141 0 8
Publications :
Sale of Transactions... csc seG seis mies os 1 3° 6
Sale of Journal, Vols. 1-6 ...........-00.- bib
9 Woliss (=12 wots secre stele eet 4 4 9
“1 Vols al3aU5 - ses com eeaetnels 4 9 0
‘ Wolks Londen sean ee 20 0
5 Welln SEJi ele sie, atodetercyw get nocsuee 11710
fs Wala Vea ec ee ee 211 0
ms Vise) WOM rs elentacietoveveustsimrensre 412 0
is Viol 20" kw dae eee 15 8 2
As NOE SQM we tae Nhe Sather eee tens 6418 7
- —————— 108 16 2
Longman and Co., Sale of Journal in 1864 ...... oo Odea
Sale of Geological Map ......2+--eeeecees 12 12 0
Sale of Library-catalogues ......-.-esseee- 1 9 G
Sale of Ormerod’s Index.......2sccccscoee 1 0 0
15 6
We have compared the Books and
Accounts presented to us, and find
them correct.
(Signed) THOS. WILTSHIRE, :
: AUPRED TYEOR (0 2

Feb. 7, 1866.

Income and Expenditure during the

Year ending December 31st, 1865.

EXPENDITURE.

General Expenditure : Ere hdle Be
WP eC cia hens fhe ne wis bis e'a ee ox (ob 18 04
BIVE-WOSUTANCE “262s etc e cece ne Palaieiieevete she, Oy
SO POLAIIVE: cies. 6: cece do eeecce scenes E194
House-repairs .......6-0. slang scieisiepaialale ase 15 0 3
NMR arc la's\ chs! aia: ace) ojaye ance: ain Siel'n's 6.010" 33 0 0
MINI tele ie: ia ose. on /vie' anys e,o'= «ic «nisin ele wie 28 17 10
Miscellaneous House-expenditure ........ 8616 5
OAIIOMETY occ co cs csie van sisinien eens seins 2413 2
Miscellaneous Printing .........seecccees 20 1 0
Tea for Meetings .....cseeccccscesscoes lila, 8

—_—-_ s_- 283

Salaries and Wages:

MAINEAME-SECTELATY soc cas cccecnesscce 200 0 0
PEI k ofa aeis a nc mie ws wis 06 isa d wie'e S60, :0
Library and Museum Assistants .......... 139 0 0
a dd Be ee 90 0 0
IE CCIM toto awa, ai Giaial o eared ace si eiaia'e e's 40 0 0
Oeeasional attendants. ...ccessessccseses 8 15 0
567
2 eee eee Sete eas Caen 53
Coe le act a's 8

Miscellaneous Scientific Expenses ................ 32

Publications :

Geolopical Map ...ccccessconcccsscecces 25 5 2
PRE ANV GINS I—G. x wstcseiessine eyes cies 2.1% 10
SIS Cae ae Aen ie 0 6 0
I oe i shlkaehesce ss a7 0G
PG ON aos) cacdlavesewones 520000 2
3) 57
Over-credited Arrears of Admission-fees in 1864... . 12
isalanuce at Banker's, Dec. 31, 1865 ............ oe Leao
Balance in Clerk’s hands, Dec. 31, 1865 .......... 228

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PROCEEDINGS

AT THE
ANNUAL GENERAL MEETING,

16re FEBRUARY, 1866.

AWARD OF THE WoLLASTON MEDAL.

Tue Reports of the Council and Committees having been read, the
President, Witttam Joun Hamitron, Esq., F.R.S., delivered the
Wollaston Medal to Sir Cuartzs Lyett, addressing him as follows :—

Sir Cuartes Lyeri,—I need hardly say that it is with very great
satisfaction that 1 find it has fallen to my lot to be the means
of placing in your hands this Wollaston Medal, which the Council
have unanimously awarded to you in recognition of the highly
important services you have rendered to the study of Geology by
your various original works, and for the masterly and philosophical
manner in which you have treated the subject, both in developing
the principles and in expounding the elements on which the science
of Geology is founded.

More than five-and-thirty years have now elapsed since you pub-
lished the first edition of the ‘ Principles of Geology,’ in which you
attempted to explain the former changes of the earth’s surface by
reference to causes now in operation, and by giving a full and de-
tailed view of the modern changes of the earth and its inhabitants.
During this period you have published no less than nine editions of
this work. In 1838 you published the first edition of the ‘ Ele-
ments of Geology,’ consisting of an expansion of the 4th Book of
the ‘ Principles of Geology,’ and containing a description of the monu-
ments of ancient changes, Geology in the strictest sense, namely, a de-
tailed account of the successive formations of the earth’s crust and
their imbedded fossils from the oldest crystalline rocks to the beds
of the Post-tertiary epoch. Of these ‘ Elements’ you published the
sixth edition last year, and I need not here repeat what I stated on
a former occasion respecting the vast amount of additional informa-
tion it contains as compared with former editions. Indeed, con-
sidering the rapid progress of geological study and the close atten-
tion you have always paid to every new discovery in all quarters of
the globe, it could not well be otherwise. It is impossible to calcu-
late the effect produced by these numerous publications; but it is

XXVIli PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

interesting to record the fact that I have read on more than one
occasion that a perusal of Lyell’s ‘ Elements’ has been the first means
of calling the attention of persons previously unacquainted with the
subject to the study of this branch of science and to the eager in-
vestigation of the geological features of the country where they
resided. |

I must also take this opportunity of alluding to the great services
you have rendered to the study of Tertiary Geology in helping to
clear away the uncertainty which prevailed before 1830 respecting
the true chronological sequence of those fossiliferous beds which in
England, France, and Italy overlie the chalk formation, and in many
of which a greater or less number of species are found identical
with recent or living forms. With the assistance of M. Deshayes
you prepared comparative lists of the fossil shells found in the
different Tertiary formations, and of the identical living species, and
you ascertained that in proportion to their greater antiquity they
invariably contained a smaller percentage of living forms. On this
you founded that peculiar classification with which your name must
ever be associated. The terms Eocene, Miocene, Pliocene, and Post-
plocene will always remain as a memorial of the services you
have rendered to geological science. And although subsequent disco-
veries have shown that the lines of demarcation between these
groups cannot be so sharply drawn as was at first supposed, and
that the breaks previously believed to exist have been filled up by
newly discovered groups of strata, it must not be forgotten that
you always anticipated that such would be the case; you never ad-
mitted the doctrine maintained by some geologists that these breaks,
both in the Tertiary and in the older formations, were the marks of real
interruptions and catastrophes breaking the regular series of events
in the geological history of the crust of the earth and of its inha-
bitants. The nomenclature which you introduced has been of im-
mense service in enabling us to arrange and coordinate the different
groups of Tertiary deposits which occur in so many localities of the
European area as well as in other portions of the earth’s surface.

Allow me once more to express the sincere pleasure and satisfac-
tion I experience in placing this Medal in your hands.

Sir Cuartes Lyert, on receiving the Medal, replied as follows :—

The list of British and foreign geologists who have received the
Wollaston Medal during the last thirty years has been honoured
by so many distinguished names that I cannot but feel highly gra-
tified that the Council has thought mine worthy of being added to
the number. I acknowledge with sincere thanks the flattering
terms in which you have spoken of my scientific labours and writings,
and I only trust that you have not greatly overrated their value. I
can at least assure you that as I grow older I become more and
more conscious of my inability to keep pace with the ever-increasing
rate at which geology is expanding, together with the numerous
sciences which are so intimately connected with it.

ANNIVERSARY ADDRESS OF THE PRESIDENT, 5:04

AWARD OF THE WoLLASTON DoNATION-FUND.

The President then addressed Mr. H. Woopwakrzp, as follows :— |

Mr. Woopwarp,—I have much pleasure in handing to you the
balance of the proceeds of the Wollaston Fund, which the Council
have awarded to you with the view of assisting you in your resear-
ches on the fossil Crustacea. The evidences of industry and zeal
which you have already shown in this field of paleontological re-
search, both in the many interesting communications which you
have made to this Society and in your other publications, lead us to
expect still more important results from your continued inyestiga-
tions. It is this division of labour which tends finally to perfection.
And while Mr. Davidson has taken the fossil Brachiopoda under his
special charge, Dr. Wright the Echinoderms, and Mr. Salter has done
the same with the Trilobites, we gladly leave the remaining Crustacea
in your hands, in the confident hope that you will treat them with the
same success, and work out their natural affinities and geological limi-
tations with the same credit to yourself and benefit to science, which
they have already manifested in their respective fields of operation.
While assuring you of my own entire satisfaction at this award, I
will only add the expression of my sincere wishes for your future
prosperity and success.

Mr. Woopwarp replied as follows :—

Mr. Presipent,—In returning thanks to you and to the Council
for the honour conferred upon me, I cannot but recall the names of
the many able and distinguished geologists who in former years have
received the Wollaston Fund, and feel sure it is owing more to your
friendly consideration than to my own desert that I am thus
favoured. _

Palzontologists have never had greater opportunities for work
than at the present time, when so many fresh districts are being
explored, yielding new series of organisms dissimilar from, but re-
lated to, the living forms around us.

We younger naturalists and geologists have an immense advantage
over our predecessors, for we enjoy the results of their labours, and
find that they have made the way light and the path smooth beneath
our feet. New fossils, however, turn up continually, and must be
described ; and better examples of old ones, furnishing fresh ma-
terial for comparison, need to be examined.

With the encouragement which you have been pleased to bestow,
I hope to add some useful material to the ancient history of the
Crustacea, which it is my pleasant task to investigate.

XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

THE ANNIVERSARY ADDRESS OF THE PRESIDENT,
Witiam Jonn Hamitton, Kse., F.R.S.

I now proceed, in accordance with the practice hitherto observed
by my predecessors, and before entering on those observations re-
specting the recent progress of geological investigation which it is
my duty to lay before you, to read the Obituary Notices of some of
those Fellows of the Society whom we have lost during the past
year.

Mr. Huyry Cristy was the second son of the late Mr. William
Miller Christy, of Woodbines, Kingston-upon-Thames, and was born
on the 26th of July, 1810. His early life was devoted to business,
and he succeeded his father as a Director of the London Joint-Stock
Bank. A taste for antiquarian researches led him, however, at an
early period to undertake many extensive journeys and expeditions
with the view of studying the antiquarian remains of various dis-
tricts, and the primitive habits and customs of the more remote
tribes of the human race.

In 1856 he accompanied Mr. Edward Tylor to Mexico. The result
of their travels was published by Mr. Tylor in 1861 m a work called
‘Anahuac.’ He subsequently visited the United States, Canada,
and British Columbia, picking up information wherever he could
find it respecting the habits of the wilder tribes and the earlier in-
habitants. Subsequently he visited the East, Algeria, and the
north of Africa, Spain, Italy, France, and the Scandinavian king-
dom.

It was at a later period, however, that he turned his atten-
tion to that branch of his antiquarian pursuits which brought him
into close relationship with this Society, of which he became a Mem-
ber in 1858. Carrying back his researches into the antiquity of ~
man’s presence on the earth, he was brought into close contact
with the relics of the last period of geological history, when Mam-
malia, now extinct, appear to have lived during the Postgla-
cial period as the cotemporaneous inhabitants in caves and forests
of the first tribes of the human race which dwelt in Western
Kurope.

The discoveries of Abbeville and of Amiens which had been so
ably worked out by Mr. Prestwich, induced Mr. Christy to enter
upon a new field of inquiry ; and, in conjunction with his friend M.
Lartét, he turned his attention to the caves in the south of France,
to which several French geologists had recently been devoting their
time and thoughts, and were endeavouring to unravel the mys-
tery which at first attached to the discovery of undoubted human
implements, and the works of human hands, in close juxta-position
with the remains of extinct Mammalia.

Mr. Christy’s exertions were chiefly directed to the examination,
with his friend M. Lartét, of the numerous caves which are to be
found along the banks of the Vezére in the Department of the Dor-
dogne. The enormous collection of materials obtained from these

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXX1

caves, consisting of flint instruments of an entirely different character
from those of Amiens and Abbeville, of bones of Reindeer, Bos, and
other animals, would appear incredible to those who had not wit-
nessed the actual discovery and the immense stores collected on the
spot. They have been distributed, with the greatest liberality, by
Mr. Christy and M. Lartét to the various public museums and pri-
vate collections in Kurope.

In the spring of last year Mr. Christy proceeded, with other Mem-
bers of the Geological Society, to visit some interesting caves of the
same character as those in the Dordogne, which had been recently
discovered in Belgium, near Dinant on the Meuse; and it was
whilst proceeding thence to Switzerland, with M. and Madame
Lartét, that he was attacked by inflammation of the lungs, which
carried him off in a few days. He died on the 4th of May, at La Pa-
lisse, Allier, at the age of 54. He will be long regretted by all who
knew him for his social qualities no less than for his scientific
attainments.

Sir Jonn Witi1am Lussock, the son of Sir John W. Lubbock, was
born on the 26th March, 18038. He was educated at Eton and at Tri-
nity College, Cambridge, where he took his degree in 1825. He was a
first-rate mathematician, and for many years was devoted to the pur-
suit of science, particularly that of astronomy, in connexion with
which he investigated many questions respecting the action of the
tides, the theory of the moon and the perturbation of the planets, and
the determination of the distance of a comet from the earth, and the
elements of its orbit. He was Treasurer to the Royal Society from
1830 to 1835, and again from 1838 to 1845, and was for many years
Vice-Chancellor of the University of London. In 1834 the Royal
Society awarded him one of their Royal Medals for his paper ‘“‘ On the
Tides,” and in 1848 the Astronomical Society gave him a testimonial
for his ‘“‘ Researches on the Theory of Perturbation.’’ In 1836 he de-
livered the Bakerian Lecture “‘ On the Tides at the Port of London.”
He was elected a Fellow of this Society in 1848. He contributed
many papers on scientific subjects to most of the learned Societies in
England, which were published in the Philosophical Transactions,
the Memoirs of the Royal Astronomical Society, the Philosophical
Magazine, the Transactions of the Cambridge Philosophical Society, °
and the Reports of the British Association.

In addition to these communications he published several import-
ant works on astronomical and mathematical subjects between the
years 1830 and 1840, including ‘ A Treatise on Probability ’ and an
‘Hlementary Treatise onthe computation of Eclipsesand Occultations,’
in 1835; ‘ Remarks on the Classification of the different branches of
Human Knowledge, in 1838; an ‘ Elementary Treatise on the
Tides,’ in 1839; and ‘ On the Heat of Vapour,’ and on‘ Astronomical
Refraction,’ in 1840. In this year he succeeded to the Baronetcy
on the death of his father, and from this period appears to have
withdrawn himself somewhat from the active pursuit of scientific in-
vestigations. That they were not altogether given up is proved by

XXXil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

the fact that he became a Fellow of this Society in 1848, in which
year he also communicated to the Society an interesting paper
“On change of Climate resulting from a change in the Earth’s Axis
of Rotation.” This paper, which derives additional interest from
the discussions which have been recently carried on, was fully dis-
cussed by. Sir H. Delabeche in his Anniversary Address of the
same year *. Sir John Lubbock died at High Elm, Farnboro’, Kent,
on the 20th of June, 1865, at the age of 62.

Mr. Nicnoras Woop was born in 1795. Having from an early
age directed his attention to mining engineering, he became one of
the most distinguished colliery-viewers in the north of England.
This did not prevent his pursuing many branches of scientific inves-
tigation, amongst the most important of which was the encourage-
ment he gave from a very early date to the introduction of the rail-
way system. He it was who first wrote upon the subject, and
showed how the tramways which had been used for local purposes
might be made available for more general travelling. Under his
auspices the Stephensons became famous and the locomotive engine
was perfected, and he will ever hold high rank wherever the science
of the nineteenth century, in the development of which he took so
great a share, is known.

In 1831 he read before the Natural History Society of Newcastle-
on-Tyne a paper ‘‘ On the Geology of Northumberland and Cumber-
land,” illustrated by a map and numerous sections, exhibiting the
true coal-fields, the Millstone-grit, and Mountain-limestone districts.
He also pointed out the effect of a remarkable dyke in dislocating
or throwing down a portion of the Newcastle coal-field so as to ren-
‘der it available for mining in a district where, in the ordinary range
of the strata, no coal would otherwise have been found. The value
of these illustrations was great in a practical point of view, and the
merit of such researches was enhanced by the comparative infancy
of the science.

In 1844 Mr. Wood proposed at a meeting at Newcastle the regis-
tration of mining operations, the importance of which, in a geological
no less than a commercial point of view, can hardly be exaggerated.
In founding the Northern Institute of Mining Engineers at Newcastle
in September 1852, Mr. Wood delivered an address which comprises a
review of many of the most important subjects connected with prac-
tical coal-winning. He was eminently practical in his views, and
it is worthy of special notice that in this address he placed geology
in a prominent position. He said that the study of Geology and all
its concomitant branches of science—Mineralogy, Chemistry, Me-
chanical Philosophy, Pneumatics, and Mechanics—are all subjects
which might usefully and profitably occupy the time and attention
of all the members of the Institution, and of the meetings of the
Institution collectively. He also added suggestions for the collec-
tion of plans and records as a means of cultivating and extending
geological science.

* See Quart. Journ. Geol. Soc. vol. v. pp. 4 and Ixxxiv.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXlil

In November 1855 he advocated the formation of a mining school,
in which naturally his attention was chiefly absorbed by the local
attractions of the North of England Coal-fields. At the same time he
recorded his due acknowledgment of the efforts made to establish
an Office of Mining Records in London, which, first taken up by Sir
Henry Delabecke, and subsequently promoted by Sir R. Murchison,
was then ripening into what it has since become—a valuable school
of mining science.

In 1855 he gave an excellent account of the sinking for coal
through the Magnesian Limestone, accompanied by detailed sections.
In 1863, together with Mr. Boyd, he prepared a geological paper on
the Wash or Drift in the county of Durham, tracing the denudation
over a great extent of country. He was elected a Fellow of this
Society in 1843, and was also a Fellow of the Royal Society. He
died on the 19th December 1865, in his 71st year.

Mr. Lovett Reeve, the son of Mr. Thomas Reeve, of Ludgate
Hill, was born April 19, 1814. After distinguishing himself at
school by his proficiency in Greek and Latin, he was at the age of
13 bound apprentice to a grocer on Ludgate Hill, where the acci-
dental arrival of a sailor with a handkerchief of shells, of which
he became the purchaser, led to his becoming an ardent student of
natural history. From this small beginning his collection gradually
increased, and in this he was assisted and encouraged by forming an
acquaintance with a Mr. Walker, a compositor, also a zealous con-
chologist, as well as with Dr. Gray of the British Museum. In
1833 he attended the third meeting of the British Association at
Cambridge, and in the Natural-History Section he was appointed
Conchologist to a general exploring-expedition into the fens between
Cambridge and Ely.

When his seven years of apprenticeship were over he proceeded to
Paris, where he made his first contribution to the literature of Con-
chology, in the form of a paper “ On the Classification of the Mol-
lusea.” This was read at a meeting of the Academy of Sciences. On
his return to London he devoted himself with increased earnest-
ness to his favourite study, and in a short time produced his ‘ Con-
chologia Systematica,’ in two 4to volumes, illustrated by 300
plates of shells, published by Messrs. Longman in 1840-41. But
the cost of publishing this expensive work exhausted his funds, even
to the sacrifice of his share in his deceased father’s property.

About this time the fortunate and almost accidental purchase of a
valuable collection of shells at Rotterdam, made with great care at
the Moluccas by the Dutch Governor, General von Ryder, enabled
Mr. Reeve to return to his favourite occupation. By these and other
means he was soon enabled to undertake the publication of an illus-
trated work on the species of shells, entitled ‘Conchologia Iconica,’
the value of which has been recognized by every paleontologist who
is aware of the importance of accurate delineation of living species

. for the purpose of comparison with specimens of extinct forms. It
was a fortunate moment when Mr. Lovell Reeve undertook this
VOL. XXII, ¢

XXXIV PROCEEDINGS OF THE GEROLOGICAL SOCIETY.

work. Mr. Hugh Cuming had just returned home from his long ex-
pedition round the world, bringing with him vast stores of Mollusca
collected during his years of wandering; many of these were alto-
gether new to science, and the publication of them was looked for-
ward to with the greatest interest both by paleontologists and con-
chologists. This great work has been continued with almost unin-
terrupted regularity since 1843 down to the present time.

In 1850 Mr. Lovell Reeve published a useful elementary work
entitled ‘ Klements of Conchology, an introduction to the Natural
History of Shells and of the Animals which form them.’ He sub-
sequently became, on his removal to Henrietta Street, Covent Garden,
the publisher of many other works on natural history, and was
afterwards the proprietor of the ‘Literary Gazette,’ which he edited
with great ability from 1850 to 1856. He became a Fellow of this
Society in 1853, and regularly presented to our Library the sueces-
sive Monographs of the ‘Conchologia Iconica.’ His last, and by some
considered his best, work, on the ‘ Land and Freshwater Mollusks of
the British Isles,’ was published in 1863. It contains mueh useful
information “ on the geographical distribution in other parts of the
world of the species indigenous to this country, and on the relation
which this distribution bears to climate, soil, and other local eireum-
stances.”” He was a man of a most amiable disposition, and bore
with exemplary patience for eighteen months the acute sufferings
caused by a most painful illness. He died on the 18th of November,
1865.

Dr. S. P. Woopwarp, the son of Mr. Samuel Woodward of
Norwich, was born September 17th, 1821. By his death the
Society has experienced a very serious loss. His sound knowledge
and assistance, both as a naturalist and a paleontologist, were always
at the service of the Society or of its Fellows. From his earliest
infancy his constitution was weak and delicate, and he showed his in-
clination for the study of natural history by beginning to form a
collection of insects before he was eight years old; and when he had
scarcely attained the age of ten years he assisted in publishing an ac-
count of the Trichiosoma lucorum in Loudon’s ‘ Magazine of Natural
History,’ with an engraving of the insect in all its stages. In the
following year he began the study of land and freshwater shells,
and commenced the formation of his father’s collection. To these
pursuits he soon added the study of botany, after which entomology
was given up, and he became a constant and zealous cultivator of
botany and malacology, which were never relinquished.

In 1838 he came to London to complete his education at the
London University, and soon obtained an appointment in the
Library cf the British Museum. In 1839 he succeeded Mr. Searles
Wood, whose health had compelled him to resign, as Sub-Curator in
the museum of this society, under Mr. Lonsdale. From this time
he added paleontology to his other studies, and laboured assiduously
in the arrangement of our collections and the improvement of the |
museum until 1845, when he was appointed Professor of Botany

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV

and Natural History, including Geology, at the Royal Agricultural
Coliege at Cirencester.

He was one of the founders of the Cotteswold Naturalists’ Field
Club, and in 1848 was appointed First-class Assistant in the Depart-
ment of Geology and Mineralogy in the British Museum. He sub-
sequently received the appointment of Examiner for the Council of
Military Education, as well as Examiner in Geology to the Uni-
versity of London. He was a constant contributor to various
scientific and literary periodicals, and the pages of our own journal
contain many valuable productions from his pen. In 1854 he
communicated to this society a highly interesting paper ‘‘On the
Structure and Affinities of the Hippuritide,”’ in which many of the
peculiar characters of these remarkable fossils were for the first time
clearly brought together. With regard to the fossils to which they
may be said to bear the closest resemblance, Mr. Woodward showed,
while repudiating the doctrine of transmutation, that 1t might be
assumed that the Cretaceous Hippurties are connected with the
Oolitic Dicerata and Tertiary Chame. After describing the struc-
ture of the Hippurites and other allied genera, of which numerous
woodcuts and plates of engravings serve as illustrations. he proceeds
to give their affinities. He points out the successive opinions of various
paleontologists, from Parkinson and others, who considered them
as Orthoceratites, to the time when Prof. Quenstedt placed them in a
more natural position, between the Chamacee and the Cardiade,
The fact of their being bivalves had already been satisfactorily
established.

In 1856 he gave us a description of a new Orthoceras from China,
one specimen of which measured 29 inches in length. They, how-
ever, occurred only as longitudinal sections in thin plates of lime-
stone, artificially worked down for some artistic or domestic purpose,
and brought from some place distant 200 miles from Shanghae.
Knough, however, of the shell remained to enable Mr. Woodward to
describe its structure and to ascertain the series of changes which it
had undergone.

In 1860 he assisted Capt. Spratt in naming the recent shells
from Bessarabia, as well as the fossil shells from the lower fresh-
water deposits of Bessarabia, lists of which are published in our
journal of that year.

He also contributed several papers to the ‘ Proceedings of the
Zoological Society,’ to the ‘ Intellectual Observer,’ and to the
‘Annals of Natural History.’ The article on Volcanos in the
‘Encyclopedia Britannica’ was written by him; and for many
years he prepared Reports on the Proceedings of the Geological Sec-
tion of the British Association.

But, perhaps, the most important and valuable work which he
contributed to science is the ‘ Manual of Recent and Fossil Shells,’
published 1851 to 1856. It is an excellent text-book, and full of
original matter. The Supplement, containing a detailed account of
the geographical distribution of living Mollusca, as well as of the
distribution in time of the fossil species, is deserving of the highest

c2

XXXVI PROCEEDINGS OF THE GHOLOGICAL SOCIETY.

commendation. He also assisted Prof. Owen in the preparation of
that portion of his ‘Palzeontology’ which comprises the Invertebrata.

His health had been gradually declining for the last few years,
and he died at Herne Bay, July 11th, 1865.

Mr. Groner Rozerts was born at Kidderminster, and for upwards
of five years held the office of Clerk to this Society, of which he
became a Fellow in 1864. He was the author of numerous papers
both on geological and other interesting subjects. These he com-
municated to the Geological Society, the ‘ Geological Magazine,’ and
other periodicals ; many of them showed great talent and boldness in
taking up original views. He died at Kidderminster, 20th December,
1865.

We have also to deplore the loss of other Members of the Society,
amongst whom I may mention the names of Samuel Cartwright,
Col. Sampson, Thomas Young, J. R. Macdonnell, F. W. Simms,
W. B. Mitchell, and T. Hutton.

Amongst the Foreign Members whom we have lost I must men-
tion the name of Dr. Curistian PanpEr, who was born at Riga

on the [th July, 1794. He was the son of a wealthy banker.

His education was commenced in the Gymnasium of his native
town. In 1812 he entered the University of Dorpat to study
medicine, but left in 1814, in order, like so many of his countrymen,
to complete his education at Berlin and Gottingen. With his great
love for natural history he became so engrossed in the study of the
preliminary sciences that he never reached the point of practical
medicine. He devoted himself to original investigations, and esta-
blished a chemical laboratory in his own house. In 1816 he went
to Wiirzburg, and there began his remarkable investigations respect-
ing the development of the chick in the egg, which led the way
to a long series of microscopical investigations respecting the
general course of the development of animal bodies. Professors
Dollinger and D’ Alton were his collaborateurs in this great work. On
its completion he undertook, with Prof. D’Alton, a long journey
through France, Spain, Holland, and England, principally with
the view of visiting the great anatomical museums of Europe, but
also for the purpose of collecting marine animals on the sea coast.
On his return home Pander was attached as naturalist to the Em-
bassy sent to Bokhara in 1820 under the direction of Baron Meyen-
dorff. In 1822 he was attached to the Imperial Academy of
Sciences of St. Petersburg, and in 1823 he became a regular
member of it in the zoological branch. While employed in sys-
_ tematically arranging the objects of the zoological collection, he
undertook the examination of the geological formations in the neigh-
bourhood of St. Petersburg, as well as their fossil remains. He
thus became, by his work entitled ‘Contributions to the Geognosy
of the Russian Empire’ (1831), the founder of our knowledge of
those formations, now called Silurian, to which Strangways and

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXVIl

Eichwald had first called the attention of geologists. In 1827 he
resigned his appointment and withdrew to his paternal property
of Zarnikau in Livonia. But even here he could not resist the
attractions of natural history. The sandy soil of Livonia contains
numerous remains of the scales and teeth of animals of a very early
period, of which the determination was most difficult. Pander col-
lected great quantities of these teeth and other fragments, and was
the first to recognize that they must have belonged to lost species of
cartilaginous fishes. But the difficulties of the position in which he
was placed, in a district where the publication of his plates was
almost impossible, and where his only object was the satisfaction of
his own scientific inclinations, led to his being anticipated by Sir R.
Murchison in making known the character of this Devonian forma-
tion with its cartilaginous fishes.

In 1842 he was appointed to the School of Mines and settled in
St. Petersburg, whence he carried out several geological ex-
peditions in Livonia, Esthonia, Central Russia, and in the Ural, the
chief object of which was to study the paleontological character of
the older formations, and to select the best spots for establishing
experimental works for coal after fixing the geological horizon
of the coal-beds of Russia. We are also indebted to Pander for
the important and practical explanations respecting the beds and

contents of the Ural coal-field. He died on the 5 oe , September, 1860,

after long suffering from a painful disorder. He will be long re-
gretted as one of the truest of friends and most Seaniecermied! and
unselfish of scientific men. Science was to him the love of his heart,
and he never could be induced to use it for the furtherance or im-
provement of his own position.

Kart von Raumer was born at Worlitz, near. Dessau, on the 9th
April, 1783. In 1797 he attended the Joachimsthal Gymnasium
in Berlin, and was at this early age distinguished for his love of
art and poetry as well as science. In 1801 he commenced his
academical career at Gottingen, where, contrary to his own inclina-
tions, he devoted himself to his legal studies. At the same time
he attended Blumenbach’s lectures, and became a great proficient in
music. He worked and read hard, and his education was at this
time literary rather than scientific. In 1803 he removed to
Halle. Here he remained a year longer than the parental pro-
gramme had originally contemplated, for the purpose of attending the
lectures of Prof. Steffens. This first awoke his love for natural
history, which subsequently became the ruling passion of his life.
Deeply interested by Steffens’s lectures on the internal history of
the earth (this was in 1805), he was greatly excited by the grand
idea therein developed, that the earth also haditshistory. He now
learnt, for the first time, that Werner had founded his history
of the development of the earth on his observations on existing
mountain forms. In 1805 he went to Freiberg to attend Werner’s
lectures, where the great naturalist gradually weaned him from his
philosophical and historical inclinations to the earnest and engros-

XXXVIl1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

ing study of mineralogy. He remained at Freiberg until 1808. At
this period of his life, at the age of twenty-three, he is described as
a most engaging and fascinating person. He became intimate with
Varnhagen and Schleiermacher, and was the constant companion of
Schubert and of Engelhardt.

The battle of Jena produced a great effect on his outer and
inner life. Overwhelmed by the sad fate of his country, he looked
for consolation, first, to his mineralogical studies, and then began
his geological explorations with Engelhardt, exploring the Erzge-
birge and the mountains on the Rhine between Cologne and Stras-
bourg, and subsequently the formations in the neighbourhood of
Paris. Here a remarkable change took place in his ideas. His
hatred towards the conquerors of his country, and the reading of
the works of Pestalozzi and others, engendered the idea of exerting
himself for the improvement of the education of young Germany,
and of raising a more fertile produce from the rotten soil.

After another visit to the Syenitic formation of the Erzgebirge,
he proceeded to visit Pestalozzi, at Yverdon, and became a teacher
in his establishment. But here a sad disappoimtment awaited him.
Only a few weeks had passed away before he was undeceived and
became aware of the total want cf method in the system, and of the
germs of destruction and decay which it contained; Pestalozzi con-
fessed it himself, and in May 1810 Raumer left him a sadder but
awiserman. In Nurnberg he again met Schubert, who encouraged
him to publish the results of his former explorations under the title
of ‘Geognostical Fragments.’ The unexpected success of this, his
first publication, led to his being appointed Professor of Mineralogy
at Breslau,in 1811, and councillor of the miming establishment
there. But this publication also bore bitter fruit, and led to a tem-
porary estrangement between him and his beloved teacher Werner.
He had proved in this work that the sequence of the beds of the older
rocks which Werner had laid down was by no means of universal
application, and that this very Erzgebirge, which Werner had con-
sidered as the type of all mountain-formations, was itself a remark~
able exception. He was himself astonished at the result, but the fol-
lowers of Werner were indignant. The quarrel was made up in 1814.

The commencement of his duties in Breslau, notwithstanding the
fact that his brother, the historian, Frederic v. Raumer, was one of
his colleagues, was attended with great difficulties, for want of a
good mineralogical collection. The investigation of the Silesian
mountains, in 1812, was a more agreeable occupation, and in 1813
he published his work ‘On the Granite of the Riesengebirge.’ But
the spring of this year brought another change. The appeal of
the king to arms for the liberation of the country found an echo
in his heart. He entered the Landwehr, became aide-de-camn to
General Gneisenau, took part in the battle of Leipzig and ‘other
minor engagements, and was employed on many important and con-
fidential missions. On the 4th of May, 1814, he was most honour-
ably dismissed by the king, and a few days afterwards was decorated
with the Order of the Iron Cross.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXX1X

He returned to his duties at Breslau, where he spent several happy
years, until the unfortunate events of 1817 and the excesses of
some of the Burschenschafts again caused troubles in his happy
circle. Raumer had ever taken a lively interest in the develop-
ment of young men, and had encouraged the use of gymnastics, or
<'Turnen ;’’ and as some of the excesses of the times were con-
nected with the gymnastic societies, Karl v. Raumer was most un-
justly looked upon with suspicion even by some of his most intimate
friends. .

This led him to seek another appointment, and in 1819 he was
named Professor of Mineralogy at the University of Halle. He had
now completed his most important geological work, ‘The Mountains
of Lower Silesia, of the County Glatz, of part of Bohemia and Ober-
lausitz, geologically represented.’ The merits of this work have been
fully recognized by all subsequent competent observers. He remained
at Halle until 1823, but even here his position was not altogether
satisfactory. This was the period of the reactionary persecution of
the so-called demagogic tendencies of the students of the German
Universities. Much as Raumer had encouraged the development of
youthful energies, no one was more opposed than he was to their
excesses ; and it grieved him to see what was, in fact, only occasional
excrescences of the new growth looked upon as the main object of
the new movement. But his protection of the students was of no
avail, and he himself was looked upon with suspicion ; this deter-
mined him to leave Halle, and for a time he undertook the manage-
ment of a private school at Nurnberg. Here he was again disap-
pointed ; circumstances over which he had no control led to the
breaking up of the institution in 1826, and Raumer again found
himself without a post. But in the following year Schubert’s re-
moval to Munich opened the way to his appointment at the Uni-
versity of Erlangen, where he passed a happy and honourable exist-
ence for the remainder of his life. His influence over the students
was great, and amongst his colleagues were many who had been his
pupils in former years. Here he published his ‘ Manual of Universal
Geography’ (‘Lehrbuch der allgemeinen Geographie’), so highly
prized by Alexander v. Humboldt ; his ‘ Palestina,’ no less highly
spoken of by Karl Ritter; and his ‘ History of Peedagogik (or science
of education) from the restoration of Classical Studies, a work of
universal estimation. His principal duties at Erlangen were to
lecture on natural history and mineralogy, for the latter of which
he formed an excellent collection. He retained his faculties, both of
body and mind, almost to the last moment of his life, and died on
the 2nd of June, 1865, beloved and regretted by all who knew him.

Having as yet failed in obtaining any obituary notice respecting
the other Foreign Members whom we have lost, I can here only
mention their names :—Charles v. Oeynhausen of Westphalia, who
will be well remembered by many of our older geologists as having
visited this country upwards of thirty-five years ago, when he explored
the highlands of Scotland and the Isle of Sky under the guidance of

xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Prof. Sedgwick and Sir Roderick Murchison; Dr. Forchhammer of
Copenhagen, born at Husum in 1794 (he was President of the
Polytechnicum in Copenhagen, and died on the 14th December, 1863);
and Dr. Oppel of Munich, who was elected a Foreign Correspondent
only two years ago: he was a Member of the Academy of Sciences,
and Conservator of the Paleontological Museum of Munich; he died
on the 23rd of December, 1865.

T shall now proceed to lay before you some account of the progress
of our science during the past year, and of the principal works which
have been published at home and abroad bearing in any way upon
the advance of geological knowledge. But here, at the very outset
of my task, I findit necessary to claim your indulgence. Were I to
allude, however briefly, to every work and every memoir to be found
in the many scientific publications of Europe and America, every one
of which contains new and interesting matter, you would only have
to listen to a dry and uninteresting catalogue. I have therefore been
compelled to make a selection of such as appeared to me most inter-
esting or important; and here it is that I must claim your indul-
gence, if I have failed in the due appreciation of their relative
merits. I cannot but fear that I may have overlooked many works
of great value, while I may possibly have given undue attention to
others less deserving of such notice. I will only add that I have en-
deavoured, as far as possible, to arrange the different notices accord-
ing to geological chronology, beginning with the oldest formations.

I must, however, preface my remarks with an account of some of
the Geological Surveys which have been carried on in different parts
of the world.

Geological Survey of the United Kingdom.

I learn from Sir Roderick Murchison that, with respect to
England, the progress made by the Geological Survey under Prof.
Ramsay chiefly relates to the south-eastern and northern counties,
483 square miles having been surveyed in the former, and 510 in the
latter. In Scotland 332 square miles have been surveyed; for the most
part in the Carboniferous strata, and in that highly metamorphosed
and difficult ground occupied by Old Red Sandstone and Silurian,
south of Ayr and Dalmellngton. These areas, with tracts of minor
extent in detached parts of England, make a total of 1500 square
miles for Great Britain.

The publication of the maps relating to the geology of England
has necessarily been delayed by the insertion in the old copper-plates
of the lines of railroad and other additions, which the public have
called for. The sanction of the Treasury having at length been
obtained, Sir Henry James is now occupied in improving the topo-
graphy of the electrotype-plates for the Geological Survey, and in-
serting thereon the lines of all railways and the degrees of latitude
and longitude.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xli

In Ireland, Mr. Jukes reports that 1037 square miles have been
surveyed, and that four new sheets have been issued, making the
total number that have been published 102.

On what may be viewed as an important new feature in classifica-
tion, it will interest geologists to know that, in considerable tracts,
extending over large parts of Somersetshire and Gloucestershire, the
Rheetic or Penarth beds are being elaborately laid down by Mr.
Bristow ; whilst, as is well known to the Society, Mr. Dawkins and
Mr. Etheridge have completed sections which accurately define the
contents and succession of the fossil remains in this peculiar deposit.

Amongst the memoirs published by the Geological Survey, none
perhaps will be found more useful than the ‘ Catalogue of the Collec-
tion of fossils in the Museum of Practical Geology,’ by Professor Hux-
ley and Mr. Etheridge, published during the past year, with an
explanatory introduction by Prof. Huxley. I would gladly have
given some account of this most interesting preface, containing a
clear exposition of some principles of natural history, as well as the
application of natural history to the study and elucidation of fossils,
or paleontology ; but to do justice to such a subject it would be
necessary to quote almost every line of every page. Such a proceed-
ing would be impossible ; it would also, I trust, be unnecessary, for
the book itself must find its way into the hands of every British
geologist at least. I must therefore content myself with recom-
mending it to your special notice, not only on account of the matter
it contains, but for its close and logical reasoning, and the pleasing
style in which it is written.

Geologuwal Survey of Canada.

As the Geological Survey of Canada progresses, under the direction
of Sir W. E. Logan, the exertions of the surveyors have been re-
warded by the discovery of many new forms of animal life. These
have been described and published from time to time by Mr.
Billings, the paleontologist to the Survey. The volume for 1865,
now before me, contains amongst other matter several articles on the
discovery of these fossils, viz. new species of fossils from the lime-
stones of the Quebec group, from Point Lévis and other localities in
Canada East. Amongst the new fossils here described is a new
Orthis, a new genus called Clisospira, Ophileta 2 species, Mur-
chisonia 3 sp., Pleurotomaria 1 sp., Cyrtoceras 4 sp., Dikelocephalus
7 sp., Olenus 1 sp., Bathyurus 3 sp., and Cheirurus 1 sp. The next
article is on new species of fossils from the Quebec group in the
northern part of Newfoundland. The north-western coast of New-
foundland, from Cape Norman to Bonne Bay, on the Gulf of the St.
Lawrence. a distance of about 180 miles, is composed altogether of
Lower Silurian limestones, slates, quartzites, and sandstones. The
width of this belt of Silurian rocks is from five to ten miles. The
fossils show that these rocks belong to the Potsdam and Quebec
groups, the former having a thickness of about 2000 feet, while the
Quebec group is about 6600 feet in thickness.

The author gives a table of the different members of this series of

xii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

rocks abridged from the measured sections published in the ‘ Geology
of Canada.’ Amongst the principal fossils here described, beginning
with the Protozoa, are Culathium, a new genus, 4 sp., Trachyum
2 sp., Stomatopora 2 sp., fragments of Crinoidea, Stenaster Hualeyt,
Lingula 3 sp., Acrotreta 1 sp., Orthis 3 sp., with portions of others,
Strophomena 2 sp., Camarella 3 sp., Rhynchonella 1 sp., Huchasma
1 sp., Hopteria 1 sp., Ctenodonta 1 sp. Amongst the Gasteropoda
are Holopea 1 sp., Straparollina 1 sp., Seba 1 sp., Pleurotomaria
12 sp., Murchisonia 9 sp., Maclurea 11 sp., and opercula of three more,
Ophileta 2 sp., Helicotoma 4 sp., Ecculiomphalus 3 sp., Metoptoma
1 sp. Of Cephalopoda, Orthoceras 8 sp., Piloceras3 sp. Of Nautilus
4+ new species are provisionally named. Amongst the new species of
Crustacea are Bathyurus 4 sp., Bathyurellus 6 sp., Dolichometopus
2 sp., Asaphus 3 sp.; Nileus 3 sp., [llenus 5 sp., Harpides 2 sp.,
Inchas 1 sp., Shumardia 1, Chetrurus 6 sp., Amphion 3 sp., Triar-
thrus 1, Telephus 1, Ener inurus (2) ie Remopleurides 2, Ampyw 4,
Agnostus 2, Entomostraca : Leper -ditia 3, Beyrichia 1.

The next article or memoir contains a description of new fossils from
the Quebec group in Eastern Canada, with some others previously de-
scribed, and some from otherformations. Most of these species were dis-
covered after the former memoir, describing the new fossils from Point
Lévis, &c. had been printed. The new species are—Lingula 1, Orthis
4, Camarella 3, Eopterra 2, Murchisoma 1, Metoptoma 1, Helicotoma
1, Ophileta 1, Bellerophon 1, Orthoceras 10, Cyrtoceras 1, Asaphus 2,
Bathyurellus 3, Amphion 2, Cheirurus 4, Remopleurides 1, Harpes 1,
Illcenus 4, Harpides 1, Calathium 1. Other species still remain to
be described ; but even the list which I have given above will suf-
fice to show how rich a mine of Silurian forms still remains to be
worked out in these old formations, and how far we still are from a
complete knowledge of their fossils.

Another interesting work which has reached us from the other
side of the Atlantic is ‘ A Preliminary Report on the Geology of
New Brunswick, together with a Special Report on the distribution
of the Quebec Group in that Province,’ by Henry Youle Hind, for-
merly Professor of Chemistry and Geology in the University of
Trinity College, Toronto. After giving in the introductory chapter
a detailed statement of all that had been hitherto published by other
geological explorers in the province, Mr. Youle Hind —s states
the result of the last season’s work.

1. He describes the approximate breadth of the Quebec group,
the great metalliferous formation of North America, in various
localities.

2. Having paid particular attention to the circumstances she
which the Albertite in Albert County has originated, he has come to
the conclusion that it is an inspissated petroleum, and that it has
originated from underlying Devonian rocks, probably of the same age
as those yielding the vast stores of petroleum in'Canada and the
United States.

3. The ascertained existence of the true Coal-measures within the
limits of the province is very important.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xl

4, The view formerly entertained respecting the granite belt
passing through the proyince must be greatly modified. Instead of
one broad belt it consists of a series of very narrow belts, with in-
tervening schists and metalliferous slates. This granite is of
Devonian age, and it is probably not an intrusive rock, but consists
of highly altered sedimentary strata. The same remark applies to
much of the granite in Charlotte, King’s, and Saint John counties,
which are also probably metamorphosed sedimentary rocks.

These views, with others of great interest, are more fully detailed in
the work itself, the first chapter of which describes the leading geo-
graphical features of the province, while the second contains a geo-
logical sketch of the same region. The sedimentary rocks of New
Brunswick belong to the following great divisions :—1, Recent and
Post-pliocene ; then a great break to 2, Triassic (?) ; 3, Carboniferous ;
4, Devonian; 5, Upper Silurian; 6, Middle Silurian ; 7, Lower Si-
lurian. All the beds below the Carboniferous have been very much.
disturbed. This chapter also contains some interesting observations
respecting the origin of granite and the different characters of the

granite belts traversing the province, many of which, while admit-
ting the intrusive character of others, the author supposes to be me-
tamorphosed or altered sedimentary strata belonging to the Quebec
group. Mr. Hind says, p. 50, “They have probably been altered
in position, and belong to the class named by Professor Hunt ‘ Indi-
genous rocks ;’ and there are valid reasons for supposing that much
of the granite of New Brunswick consists of altered sedimentary
strata, changed by metamorphism into plastic felspathic sandstones
and granitoid gneiss, then, by a further metamorphism, partly into
plastic granite and in part retaining traces of the stages of their me-
tamorphism.” He also shows, by the presence of graphite, that the
metamorphism of many sedimentary rocks was not accompanied by
a great elevation of temperature, and he concludes these observations
by this statement :—‘‘ The opinions which necessarily associate high
temperature with the occurrence of crystalline rocks, or of rocks
which have undergone metamorphic action, are no longer tenable.”
However novel these views may appear to many geologists, J cannot
refrain from saying that I believe they will ultimately prove to be
correct ;. I have long entertained an opinion that the early plastic
state offghe earth was due to aqueous rather than to igneous causes.
It is“a* question well deserving consideration, and which, I hope,
will soon be taken up by some one whose chemical and physical
knowledge will enable him to do justice to such an important
question.

The two following chapters are devoted to the consideration of the
Carboniferous series. The following details will afford some idea of
the Coal-fields of the eastern provinces of British North America :—

1. Upper Coal series, unproductive ........ 3300 feet.
2. Middle Coal series, productive ...,...... 4000. ,,
3. Lower Carboniferous or Gypsiferous series.. 6000 ,,

The base consists of red sandstone interstratified with beds of a coarse

xliv PROCEEDINGS OF THE GEOLOGICAL. SOCIETY.

calcareous conglomerate, reposing in many places, nearly horizontally,
on granite of Devonian age. Chapter V. is devoted to the con-
sideration of Albertite and the Albert shales. This remarkable
mineral, respecting the nature of which such different opinions were
entertained some time ago, is now shown to be an inspissated petro-
leum, occupying fissures in the Lower Carboniferous rocks along the
anticlinal axes, and injected from below at two distinct periods under
considerable pressure. The author concludes by showing that its
source lies beneath the Albert shales—in other words, beneath the
Lower Carboniferous series—and that it is consequently of Devonian
or prior origin, and probably proceeds from rocks of the same age
as those which yield the petroleum of Pennsylvania, Ohio, and
Canada,

The sixth chapter describes the rocks of the Devonian series, with
a full account of its vast mineral wealth, consisting of iron-ores,
copper, and argentiferous galena. These rocks are traversed by
many intrusive trap-dykes, having a general course from east to west.
Some of these traps are copper-bearing. ‘The seventh chapter con-
tains an account of the Upper and Middle Silurian series, while the
eighth describes the Lower Silurian series, of which the Quebec group
is the most important. Of this the author says :—<‘ Not only is the
Quebec group the great metalliferous formation of North America,
but its remarkable thickness (7000 feet) and complexity, coupled
with the extraordinary manner in which it was deposited and brought
to the surface, all unite to make it one of the most interesting and
important formations of the entire geological series, with perhaps the
single exception of the Coal-measures. Not only does it comprise a
great variety of useful rocks, but it contains in remunerative quan-
tities iron, copper, nickel, cobalt, antimony, lead, zinc, chromium,
arsenic, titanium, silver, and gold.” ‘There are some interesting re-
marks respecting the chemical origin of the metals of the Quebec
group, taken from Professor Hunt’s work ‘On some points of
American Geology,’ in which it is suggested that they were originally
brought to the surface in watery solutions, from which they were se-
parated by the reducing agency of organic matter in the form of sul-
phurets, or in the native state, and mingled with the contemporaneous
sediment in various forms. ‘The intervention of intense heat, subli-
mation, and similar hypotheses, to explain the origin of metallic ores
is considered to be uncalled for, and reference is made to the beau-
tiful experiments of De Senarmont and Daubrée. ‘The different de-
velopments and contents of the Quebec group are more fully deseribed
in the ninth chapter. In the following chapter much information
will be found respecting the effects of glacial action in modifying the
surface of the country, in many parts of which boulders of great size
and in considerable quantities are found. The rocks, too, are every-
where scratched, striated, and polished. In accounting for these
phenomena, Mr. Hind gives the preference to the theory of a glacial
covering rather than to the iceberg theory. A comparatively slight
elevation of the country, rising gradually to the north, would account
for all these phenomena by the theory of a glacial covering more

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlv

satisfactorily than the depression necessary to explain them under
the iceberg theory. In the latter case a depression of 5000 feet
would be required, whereas there is no evidence of any greater de-
pression than about 600 feet having taken place. The direction of
the moving mass of ice appears, on the evidence of the stri@w observed
in New Brunswick, to have been nearly north and south; but as
these striw can only show us the last record of the moving mass,
there is no reason for supposing that its direction may not have
varied under different conditions at former periods.

Geological Survey of India.

Under the able superintendence of Professor Oldham, the Geo-
logical Survey of India has .been prosecuted with as much ardour
and zeal as was compatible with the difficulties of the country and
the limited means at his disposal; this latter difficulty was, how-
ever, reduced by an increased rate of allowance for travelling expenses
haying been subsequently accorded by the Viceroy. Other difficulties
were also caused by several members of the staff being detached for
special service.

Amongst the more interesting results of the past season, as appears
from the ‘Annual Report,’ is the discovery, by Mr. Medlicott in Assam,
that, to the south of the River Brahma-poutra, there arewidely-spread
and highly valuable beds of Coal, of most excellent quality, superior to
any other known Indian coals, which offer promise of yielding a plenti-
ful supply of good fuel. In Central India, Mr. Mallet has carried
out a careful revision of the boundaries of the Vindhyan rocks to the
north of the Nerbudda valley, and has extended his survey to the
western extremity of the same valley. Mr. Hackett has completed
the geological examination of the country included in the first sheet
of the Gwalior map. Mr. Mallett and Dr. Stoliczka have been em-
ployed in working out the structure of the higher Himalayan regions.
The fossils from Spiti and Rupshu had been long known, but much
confusion and uncertainty existed respecting the exact localities
from which they were obtained ; these have now been worked out
on the spot, and the results will soon be published. It is, however,
already known that undoubted representatives of acknowledged Euro-
pean series—the Silurian, Carboniferous, Triassic, Rheetic, Lower and
Middle Lias, Jurassic (probably of three distinct periods), and Creta-
ceous—have been proved to occur in these mountain heights. The
fossils have been carefully examined, and the 200 varieties or so-
called species have been reduced to 164. Amongst the Cephalopoda
alone no less than 24 out of 54 supposed species must be suppressed,
having been already described under different names. In Bombay
the progress of the Survey has been delayed by various causes, but
much good work has also been done there. The Survey of the
Nerbudda valley has been completed, as well as of a large tract of
country south of that river. The prevailing surface-rock of the
district, except the alluvial deposits, is, as in the Deccan area, trap ;
the basement or bottom rocks are chiefly granitic or gneissic. Between

xvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

these two formations the principal beds are sandstones and limestones
of Cretaceous age; and to this series probably belongs the great
Mahadeva group of the Puch-murri Hills.

In Madras the examination of the quartzites of the Cudapah and
Kurnool districts has been satisfactorily continued by Messrs. King
and Foote.

The regular issue, at the stated intervals of three months, of the
successive parts ot the ‘Paleeontologia Indica’ has been steadily miain-
tained during the past year. The four parts issued have been in
continuation of the description of the splendid series of fossil Cepha-
lopoda from the Cretaceous rocks of Southern India. No less than
148 species have been described in this series, thus distributed :
Belemnites 3 species, Nautilt 22, Ammonites 93, Scaphites 3, Aniso-
ceras 11, Helwcoceras 1, Turrilites 6, Hamites 2, Hamulina 1, Ptycho-
ceras 3, and Baculites 3—a most remarkable fauna from a single
district. Of these, 38 are identical with species known in Europe
and elsewhere, and of these 38 species not less than 32 belong to the
Middle C-etaceous series of Europe.

Amongst the memoirs of the Geological Survey of India I will
only further allude to the geological sections across the Himalayan
Mountains from Wangtu Bridge on the River Sutlej] to Sungdo on
the Indus, with an account of the formations in Spiti, accompanied by
a revision of all known fossils from that district, by Dr. Ferdinand
Stoliczka.

I must also notice, however briefly, an account by Professor
Huxley of vertebrate fossils from the Panchet rocks near Ranigunj,
in Bengal, also published in the ‘ Paleeontologia Indica ;’ they con-
sist of numerous fragmentary and sometimes rolled bones, the ma-
jority of which are vertebre. There are, however, some teeth,
small portions of crania, with fragments of detached lower jaws.
They are of very great interest, as being the first remains of Verte-
brata yet discovered in the great group of rocks associated with the
coal-bearing formations of bengal. TLey were discovered by Messrs.
Blanford and Tween in a stratum of conglomerate-sandstone exposed
in the Damuda river near Deolli, fifteen miles west of Ranigunj. They
appear to have been probably terrestrial, certainly not marine; and
Professor Huxley is disposed to consider them as either of Triassic
age or as belonging to that fauna which will some day be discovered
as filling up the apparent break between the Paleozoic and Mesozoie
forms of life—an opinion which coincides with that already expressed
by Dr. Oldham and Mr. Blantord.

And while on the subject of Indian geology, I may here allude
to an account of the Paleozoic and Secondary fossils collected by
Col. Richard Strachey in the Northern Himalaya, recently published
by Messrs. Salter and Blanford. They are chiefly derived from Niti
and its neighbouring passes. A large proportion of the Silurian
fossils are from Guneejunga in the Chorhoti Pass, at an elevation
of 17,000 to 17,500 feet above the sea. The existence of these
fossils was first made public by Col. Strachey in a paper read before

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlvil

the Geological Society in 1851 *, in which the physical features of the
mountain district are fully described, and the generic characters of
the fossils are indicated by Mr. Salter. In the work now under
consideration Mr. Salter says, ‘‘ With regard to the Paleozoic rocks
of India so little was known at the time of Col. Strachey’s researches
that to have secured a fossiliferous base was a great stride in the
geology of India. The list of genera furnished by myself to the
paper above quoted sufficiently indicated the presence of a Lower
Silurian group, which, while its fossils agreed in general character
with those of Europe, was quite distinct in species. This fact sup-
plies another proof of the existence, at this early period, of marine
natural-history provinces like those of the present day. The sub-
division of the old ocean-fauna, easily recognizable over many areas
of Silurian rocks, becomes less conspicuous in the Devonian, es-
pecially in the upper part, and had become nearly obliterated in Car-
boniferous times.”

Mr. Salter observes that the Silurian species are all new. Of
Trilobites there are eight species, all except one belonging to well-
known European genera, the forms resembling those in our own
slate rocks ; they represent seven genera, one of which, Prosopiscus,
is new; Yentaculites and Serpulites also occur. The Cephalopoda
are but few, yet their general characters remind us of those of
other Silurian regions. Eight species are described, belonging to
six genera: Nautilus (?), Cyrtoceras, Liturtes, Orthoceras, Theca, and
Bellerophon; they are almost all from the Chorhoti Pass. The
Gasteropoda comprise ten species, representing six genera, and are
also chiefly from the same pass. The Lameliibranchiata are but few,
and represent three or four species of the genus Ctenodonta. The
Brachiopoda are here also, as Mr. Salter observes, the most abun-
dant shells of the Silurian deposit; under generic forms familiar
to every student of the older rocks, and (although identical with
none of them) representing even the common species of Wales and
Shropshire, they stamp the formation as accurately as if we could
trace the connexion of the beds themselves. This coincidence of
numerous genera, and, so far as we know, of specific groups peculiar
to the Lower Silurian, is very remarkable and satisfactory when
such remote districts are compared. Twenty-six species are here
described, belonging to the followmg genera: Lingula 2, Leptena
5, Strophomena ‘9, Orthis 6, with several varieties of O. Thakil,
besides other species not sufficiently perfect to admit of a satisfactory
description. Bryozoa are also abundant, and appear to have been
precisely of the same nature in the Indian as in the European areas:
as In our own slate rocks, the narrow bifurcating forms and broad
foliaceous species are found together. Two species of Spherospongia
occur amongst the Amorphozoa. Crinoid stems of several species
have also been found, but none perfect enough to be worth describing.
The genera Chetetes and Heliohtes have also been found amongst the
Zoophyta. ;

* Quart. Journ. Geol. Soc. vol. vii. p. 292.

xlvili _ PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

The Carboniferous fossils brought home by Col. Strachey are
neither abundant nor well preserved; nor are the collections of
M. Gerard and Prof. Oldham much better. These, as well as those
collected by Dr. Fleming in the Punjab, have already been described.
Mr. Davidson enumerates no less than twenty-eight species of Bra-
chiopoda, of which thirteen are identical with British fossils. Only
two new species are here described by Mr. Salter, Ohonetes Vishnu
and Aviculopecten hyemalis.

The fossils of the Triassic series are particularly intereseee they
are chietly Cephalopoda, representing the Upper Triassic group so
well developed in the Austrian Alps. The extended study of these
beds by continental geologists has, as Mr. Salter shows, only con-
firmed the impression they first gave, that their fossils were an in-
termediate group between the primary and secondary systems of
life. The Himalayan fossils of this age are but few; but the most
striking and common forms among them are the species most charac-
teristic of the same strata in the Alps. This opinion of Mr. Salter
has been confirmed by Prof. Suss of Vienna, who says that the Hall-
stadt beds of the Carinthian Alps have a peculiar band of dark shale,
tenanted almost exclusively by two fossils, viz. Halobia (Avicula)
Lommelt, Minst., and Ammonites floridus, Wilfen. It is singular
to find that these are the two most conspicuous fossil species m the
Himalayan series, mixed with several other decidedly European
forms, such as Ammonites Aon, A. Aussceanus, A. coangustatus, and
A, diffisus, Hauer ; and in all these cases the Tyrol and Himalayan
specimens have the minutest points of structure identical. The
Natica subglobulosa and the two species of Orthoceras are also identical.

In the case of the Brachiopoda, probably the inhabitants of deeper
water, it is shown that the characteristic shells Athyris Deslong-
champsui, A. Strohmeyeri, Rhynchonella retrocita, and Waldheimia Stop-
pani are all identifiable, and were easily recognized by Prof. Suss,
who has described them. The same forms occur m the Spiti Pass,
and Prof. Oldham has found in that region a great distinction be-
tween the lower mass of strata inclosing the Triassic fauna and that
above it, which is loaded with Oolitic and Triassic types.

Mr. Salter here figures a remarkable fossil brought home in abun-
dance by Dr. Gerard from the same locality, closely allied to, if not
identical with, Spirifera Keilhavii, Von Buch, a shell characteristic of
the Mountain-limestone in Arctic regions.

Thus we find the Triassic rocks of India not only forming, as it
were, a link between the Paleozoic and Secondary rocks, but con-
taining many species identical with those of the more northern
regions of Europe. Undoubtedly there is much in this to confirm —
the opinion so often entertained by paleeontologists, although it may
sometimes have been carried too far and maintained too “dogmati-
cally, namely, that in the earlier stages of organic life the same species
were more widely distributed than at present, and that over wide-
spread areas there was less variety of form, both of species and of
genera, than we meet with now. Nor is it a sufficient answer to
this theory to say that the older formations are difficult to explore,

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlix

that many forms may have been destroyed by subsequent metamor-
phism, and that we must be necessarily ignorant of most of the
species which existed in the earlier periods of the world’s history. To
a certain limited extent such may be the case ; but if there really
existed in the Paleozoic period the same diversity of form in distant
areas as we find prevailing in the present day,.it would be a strange
coincidence, and contrary to every doctrine of probability, to find
among the forms which had escaped destruction, and which had
come under the notice of the geologist, precisely those which were
either identical or analogous in different areas. Is it not, on the
other hand, more probable that during the Paleozoic period, when
the first sedimentary deposits were formed in the waters of the
ocean, the conditions of life were more similar over a larger portion
of the earth’s surface than during any subsequent period, when
partial disturbances, dislocations, and other changes had destroyed
that uniformity which at first prevailed?

But I must return to the Himalayan fossils. Mr. Salter pub-
lishes a list of the fossils from the Upper Triassic (Keuper) rocks in
the Himalayas, with the respective localities in Europe of such as
are identical; from which it appears that, out of thirty-six species,
fourteen occur in the Keuper beds of the Austrian Alps. Amongst
the species described are—Ammonites 11 species, Orthoceras 1, Na-
tica 1, Monotis 1, Pecten 2, Lima 1, Exogyra 1, Athyris 2, Rhyncho-
nella 1, Waldheimia 1, Spirifera 2. Mr. Salter remarks on the sin-
gular fact that scarcely one of the Triassic fossils obtained from the
Spiti district, and brought home last year by Prof. Oldham, corre-
sponds with those of the Niti Pass, though 100 miles nearer to the
Alps. He suggests that in the Spiti valley we may probably have
a different and an older group.

The Cephalopoda of the Jurassic rocks are next described by
Prof. Blanford of Calcutta; they consist of nineteen species, of
which eighteen are Ammonites and one a Belemnite. The identity
of Indian species with those of Europe does not appear so great as
in the case of the underlying rocks. The author says that, with
the exception of Ammonites biplex, Sow., and A. triplicatus, Sow.,
no well-identified European species occurs among Col. Strachey’s
fossils, although many of the latter are closely allied to European
types.

Mr. Salter then proceeds to describe the Gasteropoda and Bivalves
from the same range of strata; these, however, are of great thick-
ness, and, as he observes, probably include several members of the
Jurassic series. The fossils here described are—TZurbo 1 sp.,
Chemntza 1, Ostrea 2, Avicula 1, Monotis 1, Pecten 6, Inma 2,
Inoceramus 1, Modiola 1, Myophorial, Nucula 1, Mactromya 1,
Cardium 1, Astarte 1, Cuculleal, Anatina 1,*Terebratula 3, Rhyin-
chonella 2. The work concludes with an interesting postscript by
Mr. Blanford, referring to the works of Prof. Oppel and Dr. Sto-
liczka, the latter of whom has recently visited the Spiti valley, and
has made a more complete examination of the fossiliferous forma-
tions of that part of India than had been accomplished by any pre-

VOL, XXII, d

i PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

vious visitor; he also corrects some errors of nomenclature which
had crept into former notices, and refers to some discussion which
had arisen respecting the authenticity of certain specimens. He
also observes that the Spirifera Rajah, supposed to be identical with
S. Keilhavit, does not occur in the same beds with Triassic Ammo-
nites, but in beds decidedly below them, and is therefore probably of
the same relative age as the “‘ Carboniferous” of Europe. ‘The
work is illustrated by 23 plates of fossils, in which all the new
Species are engraved.

Another Valen of the works of the Palsontograsialil Society
has been published during the past year (vol. for 1863), containing
portions of four monographs. The first is the continuation of Mr.
Salter’s ““Monograph of British Trilobites,” and specially the second
part, which contains the Silurian and Devonian forms, with 8
plates. The genera here discussed are—Amphion, Staurocephalus
3 sp., Deiphon 1, Calymene 9, Homalonotus 13. The author then
commences the group of the Asaphide, of which only one species
of the genus Ogygia is here described.

The next work is the second portion of the sixth part of Mr. Da-
vidson’s “‘ Monograph of British Brachiopoda,” viz. the Devonian,
with 11 plates. The genera described in this part are—Atrypa 3 sp.,
Rhynchonella 16, Camarophoria 1 (Mr. Davidson is disposed to con-
sider this to be the same species as Prof. Phillips’s Terebratula rhom-
boidea and the Permian form C. globulina, Schlot.), Pentamerus 2,
Davidsoma 1, Strophomena 1, Streptorhynchus 4, Leptena 3, Orths
5, Chonetes 2, Strophalosia 1, Productus 4, Discina 1, Langula 1,
Calceola 1. In concluding this monograph Mr. Davidson observes
that 91 so-called species “have been described and illustrated, but
of these only 65 have been named with certainty; 14 more are
probably good species, but they are not yet sufficiently made out ;
the remaining 12, indicated merely for the sake of reference, will
probably have to be placed as synonyms of some of the other 79
species. He- then points out which of these species extend up-
wards into the Carboniferous beds, and concludes with some inter-
esting observations on the geological, geographical, and-paleonto-
logical distribution of the species, and on the sequence of the dif-
ferent beds of the Middle Devonian group, which, as well as those of
the Lower Devonian, are extr emely complicated.

The third paper in this volume is the commencement of a valuable
“‘ Monograph of British Belemnitide,” by Prof. Phillips. His memoir
commences with an historical account of the progress of discovery
respecting this group of Cephalopoda from the time when Belem-
nites were first so called by Georgius Agricola in 1546, when {they
were considered as of animal origin, down to the period of the more
recent discoveries of Buckland, Owen, and Mantell, when their true
place in nature, as belonging to the great family of Cephalopoda, was
satisfactorily established by the discovery of specimens in which the
fossil ink-bag and other characteristic parts of the animal and its
sheath have been preserved.

Prof. Phillips then proceeds to describe the structure of the Be-

ANNIVERSARY ADDRESS OF THE PRESIDENT. li

lemnitide. The most commonly preserved portion in the fossil state
is the posterior or caudal portion of the guard or sheath, which
was originally considered as the Belemnite par excellence, until it
was subsequently discovered that as this guard extended forwards
it formed a conical cavity filled with a shell of similar form, gradu-
ally expanding forwards, divided by many shelly plates,and pierced
by a small pipe or siphuncle near one edge. This is called the
phragmocone, and is rarely found complete ; when such, however, is
the case, itis covered by a thin conical shell distinct from the sub-
stance of the guard, and called “ conotheca” by Huxley. With
regard to the guard itself Prof. Phillips observes, that it is neces-
_ sary that it should be carefully observed in three distinct aspects,
viz. the dorsal and ventral faces, as well as along the axis or
apical line. Although specimens are extremely rare in which the
phragmocone and guard are found together completely, yet in spe-
cimens from the Lias of Lyme Regis and of Yorkshire the structure
of the phragmocone in relation to the guard has been sufficiently
ascertained to justify a restoration of the whole shell.

The author then proceeds to describe the classification of the
Belemnitide, but this chapter is unfinished; and no plates or
illustrations, except woodcuts, are given in this portion of the mono-
graph.

The next paper is the “ Monograph of the Fossil Reptilia of the
Liassie formation,” by Prof. Owen: part first, Sauropterygia. The
work commences with a detailed account of Plestosawrus dolicho-
dewrus, followed by P. homalospondylus, P. rostratus (Owen), and P,
rugosus (Owen), and is accompanied by 16 plates. The merit of
these osteological papers of Prof. Owen is so well known that it is
unnecessary for me to say more than that the detailed description
_ appears to exhaust whatever can be said respecting these extinct rep-
tiles, their mode of entombment, and the resulting positions in which
they have been found.

Although I do not, as a rule, purpose alluding to the papers which
have been read at our evening meetings, yet there are some which
appear to be of sufficient interest to justify my noticing them on the
present occasion. The organic structure of the Hozodn Canadense
to which I alluded last year, has been called in question by
Prof. W. King and Dr. Rowney in a paper recently read before the
Society. Having examined numerous specimens of Kozodnal Ser-
pentine from various localities, the authors consider that the ap-
pearances which Dr. Carpenter and others have pronounced to be
organic, and closely to resemble foraminiferal structure, are purely
of mineralogical origin. They consider the “skeleton” to be iden-
tical with the euleavbons matrix of certain minerals, as Chondrodite,
Pargasite, &c. The “proper wall” of the chambers is not an in-
dependent structure, in their opinion, but only the surface-portion of
the granules of chrysotile crystallized into an asbestiform layer.
The dendritic and other forms which were described as repre-
senting the “canal system,” are considered by them to be tufts of
metaxite, or some allied variety of chrysotile ; and wy and other

2

li PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

forms are, in their opinion, nothing but imbedded imitative crystal-
lizations, quite distinct from the foraminiferal structure with which
they have been compared. From these and other considerations
they conclude that Eozodnal Serpentine is a metamorphic rock, and
they throw out the suggestion that it may, in many cases, have
also undergone a pseudomorphic change—that is, it may have been.
converted from a gneissoid calcareous diorite by chemical introduc-
tions or eliminations.

Dr. Carpenter maintains the correctness of his former views.
In a paper read on the same evening he showed that a recent
siliceous cast of Amphistegina from the Australian coast exhi-
bited a perfect representation of the “asbestiform layer.” He
then showed that this asbestiform layer exhibited in Hozoon a series
of remarkable variations, which can be closely paralleled by those
which are found in the course of the “tubuli” in the shells of
existing Nummuline foraminifera, and are associated with a structure
exactly similar to the lacunar spaces intervening between the out-
side of the proper wall of the chambers and the intermediate skeleton
by which they became overgrown, formerly inferred by the author
to exist in Calcarina. With regard to the opinions advanced by
Prof. King and Dr. Rowney, he stated that even if the dendritic
passages hollowed out in the calcareous layers, and the arrangement
of the minerals in the Kozodn limestone could be accounted for by
inorganic agencies, there still remained the Nummuline structure of
the chamber-wall, to which no parallel can be shown in any un-
doubted mineral product.

The question is certainly one of great importance, and, considering
the minute microscopical structure and the mineral as well as me-
tamorphic change which the rocks have undergone, it is still in-
volved in some obscurity. It were much to be desired that the
gneissoid rocks from other localities should be carefully ex-
amined ; for if the organic theory be true in the case of old Lau-
rentian gneiss, we ought to expect a fuller confirmation of it in the
eneissic rocks of a still younger age. And though it may perhaps
be considered rash in one who has not examined the various speci-
mens microscopically beyond seeing some of Dr.Carpenter’s prepara-
tions, I am bound to say, almost against my own convictions, that
the balance of argument at present is in favour of the views laid
down by Dr. Carpenter, Dr. Dawson, and Mr. Sterry Hunt. I should
add that Dr. Carpenter also stated that he had recently detected
Eozoon in a specimen of Ophicalcite from Bohemia, in a specimen of
eneiss from near Moldau, and in the serpentinous limestone from
Bavaria.

With reference to this subject, Prof. A.Sismonda has published an
account of some organic impressions found on a mass of gneiss de-
rived from one of the boulders in the diluvium which overlies the Lias
formation north of Rezzago in the Brianza. This block must have
been brought down from the Alps, and Prof. Sismonda considers
that it probably came from the Valtellina, the mountains of which
consist of this same form of gneissic rocks, When first discovered,

ANNIVERSARY ADDRESS OF THE PRESIDENT. Vin

~ some years ago, it was supposed to be an insect; but more careful
investigations recently made, particularly by M. Brongniart, whom
he consulted, have proved it to be of vegetable origin. M. Brong-
niart concluded that it was a portien of an Hquisetum, very analogous
to LE. infundibuliforme, of the Carboniferous period, but possibly a
new species. From these considerations Prof. Sismonda concludes
that the gneiss in question is a metamorphic rock of the Carboni-
ferous period, and suggests the propriety of further search for fossil
remains in these crystalline rocks of the Alps.

M. Barrande has published, during the past year, a second volume of
his important work on the Silurian System of the centre of Bohemia.
It is the first series of the Cephalopoda, and consists of 107 plates with
corresponding explanations. In ashort preliminary notice M. Barrande
states that the Silurian Cephalopoda of Bohemia will occupy 350
plates; this large quantity of matter renders it necessary to publish
them in separate large numbers or livraisons. The present number.
forms the first series of the plates devoted to this class. It contains
about 200 species, representing the ten following genera:—Goniatites,
Nothoceras, Trochoceras, Nautilus, Gyroceras, Hercoceras, Lituttes,
Phragmoceras, Gomphoceras, and Ascoceras. The two other genera,
Orthoceras and Cyrtoceras, which complete the family of the Silurian
Nautilide of Bohemia, are much richer in species, and will fully
occupy the plates of the second and third series, with the exception
of such as will represent the features of the general study of the
Nautilide. The text belonging to these ten genera will be shortly
published ; the author has therefore confined his observations on
them, for the present, to a tabular statement pointing out their ver-
tical distribution in the different formations and their principal sub-
divisions.

One of the most remarkable results of an examination of this ta-
bular statement is the great preponderance of forms which are
characteristic of the formation, or étage, HK. Of 202 species here
figured, 155 belong to this formation, and only 47 to G, 8 to F,
and 2 to D, and at the other end of the series only 2 to H. Looking
at individual genera, out of 70 species of Gomphoceras, 61 belong
to the formation E. The only remarkable exception to this rule is
the genus Goniatites; out of 17 species, 15 belong to the formation G,
which, with the formations E, F, and H, belong to the Upper Silurian
System, and constitute M. Barrande’s “ faune troisiéme.” Besides
this wonderful development of Cephalopoda in this Upper Silurian
System of Bohemia, their rapid diminution is no less surprising.
Only two species remain in étage H, a Goniatite and a Gyreceras, and
these are only found in the lowest subdivision of the étage.

M. Barrande has also published during the past year a third
part of his work entitled ‘ Défense des Colonies,’ comprising a
general consideration of the étages G and H, with special refer-
ence to the neighbourhood of Hlubocep, near Prague. ‘The ne-
cessity for this publication, is stated to be the erroneous views en-
tertained by MM. Lipold and Krejci respecting the stratigraphical
conditions of the neighbourhood of Hlubocep and Litten. I shall not

liv PROCEEDINGS OF THE GEOLOGICAL SOCTETY.

presume on this occasion to discuss the general question of M. Bar-
rande’s Colonial System, but shall endeavour to confine myself. to a
general sketch of the contents of the work and of the objects which
he hasin view. The étages Gand H, it is well known, represent the
upper portions of the Upper Silurian formation, or the “ faune troi-
siéme”’ of M. Barrande. The work is divided into two parts; the
first is devoted to the general description of the étages G and H on the
surface of the Bohemian basin. The first two chapters give the
results of his stratigraphical and paleontological investigations with
regard to these two groups and their subdivisions. In the third chap-
ter he points out their topographical extent, and shows their horizon-
tal and vertical relations by means of two sections across the upper
division and the zone of the colonies, the one following the valley
from Tachlovitz to Radotin, and the other through the quarries of
Dvoretz and Branik, near Prague. In the fourth chapter the author
endeavours to ascertain whether the étages G and H are represented
in the Silurian basins of other countries; and in the fifth chapter he
discusses the connexions which exist between the fauna of the étages
G and H and the Devonian fauna. The second part contains an
account of his special observations respecting the phenomena of the
étages G and H in the neighbourhood of Hlubocep, with remarks on
the adverse criticisms of MM. Lipold and Krejci respecting the
stratigraphical arrangement of the beds in question.

The colonial system of M. Barrande is too well known to geolo-
gists to render it necessary for me to make any further allusion to
it than to refer you to the last edition of Sir R. I. Murchison’s
‘Siluria,’ p. 400. The anticolonial argument which MM. Krejci
and Lipold have brought forward, founded on the stratigraphical
appearances of the different formations in the neighbourhood of
Hlubogep, is thus stated by the author :—

1. There are evident dislocations at Hlubocep in the étages G
and H. ;

2. These dislocations have produced a mechanical intercalation of
the schistose beds of H amongst the limestones of G, showing
appearances perfectly resembling those of the colonies.

3. The colonies are therefore naturally explained by simple dislo-
cations and mechanical intercalations.

These statements M. Barrande emphatically denies. He shows
that the supposed existence of these dislocations is solely founded on
a want of careful observation. Independently of the synclinal fold
already pointed out, along the axis of the basin, and the anticlinal
fold, now described in the heights of Divei Hrady, these pretended
dislocations and their supposed effects are purely imaginary.

Nor does the locality of Hlubocep offer any intercalation what-
ever of the schists of H amongst the limestones of G; on the
contrary, this locality shows on each side of the synelinal axis of
the valley the regular and symmetrical series of the formations of
the étages G and H, without any appearance of mechanical origin
which could reproduce the stratigraphical and paleontological alter-
nation of the colonies. The series of formations near Hlubocep is of

ANNIVERSARY ADDRESS OF THE PRESIDENT. lv

a purely sedimentary and normal origin, independent of all disloca-
- tion or disturbance of the ground.

The process by which the author supports his views may be suc-
cinctly stated as follows:—He shows, in the first place, that the
étage G consists of three subdivisions, the lowest, g 1, being a purely
calcareous bed, g 2 being a band of argillaceous schists with calca-
reous nodules, passing, by a gradual increase of the calcareous ele-
ment, into the overlying bed g 3, consisting of limestone resembling
altogether the bed g 1, the whole forming such a complete system of
superposition and gradual passing of one into the other, as alto-
gether to preclude the possibility of the bed g 2 being an intercala-
tion of the overlying étage H, which consists entirely of argillaceous
schists. This étage is also separated into three subdivisions, h 1, h 2,
and h 3, in which the calcareous element appears to be altogether
wanting. There is no gradual passage between G and H;; the tran-
sition is sharp and well defined.

The author then proceeds to describe the palzontological contents
of the étages G and H, and their subdivisions. By these means he
has been enabled to point out the true distinction of the different
beds, for which the petrographical and stratigraphical evidence alone
was not sufficient. Thus the two calcareous bands g 1 and g3, so
closely resembling each other in a petrographical point of view, are
shown, by the numerous tabular statements of their respective
faunas, to be entirely distinct. These tables show that, with the
exception of the Cephalopoda, all the classes (p. 55), including the
Fish, Crustacea, Pteropoda, Gasteropoda, Brachiopoda, Acephala,
Radiata, and Vegetables, are represented by a much larger number
of species in g 1 than ing3. On the other hand, the Cephalopoda
are more numerous in g 3 than in g 1 in the proportion of
3 to 2; and, moreover, in bed g3 the Cephalopoda alone contain
about four times as many forms as all the other classes together
in the same bed; besides which these two beds contain very few
Species common to both.

With regard to the four schistose beds, g 2,h1,h 2, and h 3, the
distinction is equally clear; h2 andh 3, being unfossiliferous, are
easily separated from the others; and with regard to g2 andhl,
although they contain eleven species common to both, a much greater
number of species are peculiar to each.

Peculiar to g 2. Peculiar to 41.

Trlobites ...... Sr abies: Maske oy, 0
Pephalepade is. 4.5 <seres- if
Pteropoda...... | EE Ses 0
Gasterapowanc. o. Bs cones wie 0
psehrenoday oo. Ge 6 ij ale ee ais Bi
Acephala,,,.... GE die rte 3
Radiata. iy a5 ys ZG en eee 0
Vegetables i eee ae ae 2

27. 7

lvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

But these two formations are also easily distinguished by their
rocks; the schists of g 2 contain numerous calcareous nodules of a
light colour, which are altogether wanting in the bed 41, where the
calcareous element only appears at its base in thin bands, and with .
an entirely different petrographical character from that of the
nodules above mentioned. ‘Thus there is sufficient evidence to pre-
vent the possibility of mistaking these two beds, g 2 and h1.

In the next chapter (8rd) the author describes the stratigraphical
relations between the étages G and H and the other étages of the Bo-
hemian basin. The different sections from various localities are given
in great detail, and several faults are described, the explanation of
which, when the adjacent beds were unfossiliferous, was a work of
much labour and time. I must refer you to the work itself (p. 102)
for an account of the fault of Branik and the adjacent colony of
Branik, where, in the midst of the étage D5, consisting of unfos-
siliferous beds of grey schists and quartzites of great thickness, thin
fossiliferous bands occur, more or less charged with calcareous
matter, containing several species of fossils, which peculiarly charac-
terize the lower beds of étage G; thus, according to Mr. Barrande’s
theory, foreshadowing by colonization the future characteristic popu-
lation of the overlying beds. Other colonial appearances are de-
scribed, as well as a section showing the complete series of the thin
bands of étage G, with the overlying étage H, in regular conformable
stratification.

In the fourth chapter the author enters into a detailed consider-
ation as to how far the ¢étages G and H are represented in other
Silurian basins. The countries thus noticed are England, Russia,
Sweden, Norway, Thuringia, Saxony, Franconia, the Harz, France,
Spain, Sardinia, and the United States of America.

M. Barrande observes that he still adheres to the opinion, pub-
lished in his ‘ Notice préliminaire,’ and confirmed twelve years ago
in his ‘ Esquisse Géologique’ (Syst. Sil. &c., Book I.), that, although
there was a complete gencral correspondence between the great
Silurian divisions of Bohemia and England, a more detailed compari-
son of local forms proves that the different étages in each country
did not correspond with each other. Comparing the Upper Silurian
formation of England with the fawne troisiéme of Bohemia, viz. the
étagesE,F, G, H, he says that the fossils which characterize the upper
division in England and in Bohemia, taken as a whole, constitute,
both by their “analogies and their identities, whether generic or
specific, one simple general fauna, which he calls “< faune troisiéme.”
At its commencement in each country this fauna shows a close and
intimate resemblance; but, owing to local conditions, or other
unknown causes, 1t has undergone in each country a different
development, as is shown both by the unequal distribution of each
class and by the modifications caused by the extinction and pro-
eressive renewal of species. The consequence of this divergence
gradually increasing in time has been, that the beds which form the
upper portion of the upper division are connected together by a
minimum of paleontological relations, so that no individual paral-

ANNIVERSARY ADDRESS OF THE PRESIDENT. lvii

lelism can be established between them, although they all belong
to the same period of time, during the deposition of the Silurian
system.

The author then gives a table showing the vertical distribution of
57 Upper Silurian species which haye been recognized as identical
in the two countries, and shows that out of this number belonging
to the “ faune troisiéme,” 32 had already existed in the lower divi-
sion, or “faune seconde,” of England, whereas none of them are found
in the “‘faune seconde” of Bohemia; this fact alone he considers
sufficient to prove the possibility of his colonies, as these 32 species
coexisting with the ‘‘ faune seconde” of Bohemia might have immi-
grated into the Bohemian basin and have dwelt there temporarily
during the existence of this fauna. Of these 57 species, 50 occur in
the Wenlock beds and 27 extend into the Ludlow beds, whereas in
Bohemia 51 of them are found in the étage E, and only 12 appear
in étage F; only five extend into étage G and one into H. Thus
showing that étage E contains almost all the paleontological con-
nexions hitherto recognized between the “ faune troisicme” of Eng-
land and Bohemia, whereas the few identities occurring in the
three étages F, G, and H, merely serve to show that they are really
constituent parts of the same Upper Silurian division.

After describing the different connexions between the “ faune
troisiéme ” of Bohemia and the other countries mentioned above, the
author observes that these comparative statements are the only
means available for ascertaining how far the last phase of the Bohe-
mian “ faune troisiéme ” contained in the étages G and H is repre-
sented in other countries. By way of comparison, he enounces the
chief distinctive characters of this phase as follows :—

1. Intermittent or sporadic presence of fish, and particularly the
armoured type, the first appearance of which belongs to étage F.

2. Predominance of the genera Dalmanites and Bronteus amongst
the Trilobites, and the presence of the genus Calymene. The genus
Dalmanites is only represented by the group of D. Hausmanni.

3. The reappearance and relatively new development of the nau-
tiliform Cephalopods generally, and particularly of the genera Phrag-
moceras and Gomphoceras, characterized by their contracted opening.

4, Development of the group of Nautilina, representing the genus
Gomatites, which made its first appearance in the étage F.

5. Sporadic appearance of Cardiola retrostriata in the étage H.

These characters are nowhere found all together in any horizon of
the Upper Silurian division in the Paleozoic regions of the two con-
tinents; but their absence shows itself in very different degrees in
the different countries compared with Bohemia. In the neighbour-
ing regions of Saxony, Thuringia, and Franconia no trace has hitherto
been found of the last phase of the “ faune troisicme,” whereas the
earlier phase has now been distinctly recognized. The Silurian
deposits of these regions appear to belong to the great Paleozoic
zone of the north, as England, Russia, and the Harz, the faunas of
which, notwithstanding their greater distance, bear a very marked
resemblance to the phase of the étages G and H. Sweden and Nor-

lvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

way are in the same category. France, Spain, and Sardinia, although
showing clear evidence of the existence of the first phase, are also
deficient of all trace of the last phase, only in France the forma-
tions which are classed as Lower Devonian contain numerous fossils
similar to the forms found in the different étages E, F, and G.

In England, the Isle of Oesel, and the Harz, the characters of the
fauna of the étages G and H are partially represented; but in
England, amongst the six genera of fish found in the Ludlow and Pas-
sage-beds, there are none of the cwirassés or armoured types. The
Trilobites are almost entirely wanting; the Dalmanites of the
groups D. Hausmann and Bronteus are not represented. The same
is the case with the Nautilide with the contracted mouth. Gonia-
tites are unknown, as well as Cardiola retrostriata.

The United States of America form another category, showing
the principal characters which distinguish the fauna of the étages
G and H, viz., the sporadic appearance of the armoured fish, the
existence of the genus Calymene amongst the Trilobites, a greater
development of the Dalmanites type, and the reappearance and re-
lative abundance of the Nautilidz; thus the most complete repre-
sentative hitherto known of the étages G and H is found in the
State of New York.

The fifth chapter is devoted to the consideration of the connexion
between the étages F, G, and H of the Silurian basin of Bohemia
and the Devonian formations. After alluding to the evidence which
he has given that the lower calcareous étage EK contains by itself a
fauna almost as complete as that which is distributed in different
beds in other countries between the Lower Silurian and the Devo-
nian, the author proceeds to show that it would be a great error to
suppose that the upper étages F,G, H could belong, at least par-
tially, to the Devonian period. He shows, by carefully analyz-
ing the different classes of fossils contained in these three étages,
that, although they certainly do contain some species common
to the Devonian fauna, they are totally deficient in those forms
which have hitherto been considered as essentially characteristic of
the three subdivisions of the Devonian system, and that, on the other ©
hand, they contain many forms of a true Silurian character.

The result of this examination shows that although the typical
forms of many Devonian species made their first appearance in the
Silurian formation, and although, as in the case of the Nautilide, the
analogies brought forward would appear to show a greater connexion
between the Devonian faunas and the étage K than with the étage
G, no identical species, either of Trilobites, Nautilide, or Goniatites,
occur in the two formations; the same may be said of Pteropoda and >
Gasteropoda. Of Brachiopoda there are 2 species common to étage
G and the Devonian beds. Cardvola retrostriata is a remarkable
instance of connexion between the Devonian phase and the youngest
Silurian phase, as well as between the older and younger phases of
the Upper Silurian ; and M. Barrande thus sums up the result of his
examination :—

1. The last phase of the “faune troisieme” contained in the étages

ANNIVERSARY ADDRESS OF THE PRESIDENT. lix

.G and H is more or less closely connected in all classes of fossils
with the former phases of this fauna contained in the underlying
étages Ki and F,

2. Notwithstanding certain general connexions between these
same upper ¢étages, G and H, of the basin of Bohemia and the three
great Devonian subdivisions, there is no such affinity between the
faunas of the two formations as would justify our considering them
as representing, under different appearances, contemporaneous de-
posits. And with regard to the apparent paradox that the “ faune
troisiéme”’ during its later phase, nearest in point of time to the
Devonian fauna, is less closely connected with it than with the
lower étages E and F, he observes that his investigations prove that
each class of fossils shows a greater or less number of specific
connexions, without counting the constant generic connexions be-
tween the étages Hand F and the overlying Gand H; and consequently
that, in a paleontological point of view, the étages G and H completely
maintain their Silurian character, and are only associated with the
Devonian beds by those ordinary points of resemblance which occur
during any given geological epoch to announce the following period.
I haye already pointed out the object of the second portion of this
work; but I cannot take leave of M. Barrande, to whom I fear I
have hardly done fulljustice, without making one observation.

Whether the colonial theory of M. Barrande be right or wrong,
it is impossible not to see in all his observations a confirmation of
that argument which has often been supported in this room, and to
which I have myself more than once ventured to allude, viz., that
in formations of the same age, although separated geographically by
greater or less distances from each other, we must not expect to find
the same species or even genera always appearing at any given
geological horizon simultaneously. The various conditions of life,
the depth of the sea, the different proportions of calcareous or
siliceous or argillaceous elements in the deposit, must have pro-
duced a difference in the organic contents of the formation—a
difference which may often have shown a greater intensity in neigh-
bouring regions than in such as are separated by greater distances
in space. The difference caused by distance in time has always
been appreciated by geologists; but that caused by distance in space
has sometimes been overlooked, not so much perhaps of late years as
formerly, when the identity or non-identity of fossil contents was
looked upon as the all-sufficient reason for synchronizing or sepa-
rating formations occurring at a considerable distance from each
other.

Amongst the more important discoveries of last year I must
notice that of Professor Huxley, who, in examining some reptilian
remains found in the Kilkenny Coal-field, ascertained the exist-
ence of not less than six genera, five of which are certainly new,
while the sixth, according to Profesor Huxley, may or may not be
identical with the Anthracosaurus of the Scotch Carboniferous rocks.

lx PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

The five new genera have been defined in a notice communicated -
to the Royal Irish Academy by Dr. Wright, on behalf of Professor
Huxley and himself, under the names of Urocondylus, Ophiderpeton,
Ichthyerpeton, Keraterpeton, and Lepterpeton. Ophiderpeton is re-
markable for its extremely elongated and snake-like form; Icthyer-
peton for its fish-like body and short limbs ; while Urocondylus, Ke-
raterpeton, and Lepterpeton have Salamander-like forms and well-
developed limbs. In all, the vertebre are abundantly ossified, and
there are no traces of persistent branchial arches, so that they pre-
sent very important differences from Archegosaurus. The authors
then show that four of these five genera present unmistakeable re-
mains of the ventral dermal armour characteristic of the Labyrin-
thodonts, and that from this and other circumstances there can
be little doubt that they all belong to that group of extinct Am-

hibia.

: Professor Huxley informs me that, up to the time when these di-
scoveries were made, eight genera, in all, of higher organization than
fishes were known to occur in rocks of Carboniferous age in Europe,
and five in America. Of the eight European genera, only Archa-
gosaurus, Pholidogaster, and Anthracosaurus were known by more
than mere fragments ; nor do we possess at this moment a know-
ledge of the nature of the limbs in any one of these genera, except
Archegosaurus. The five American genera Baphetes, Raniceps,
Dendrerpeton, Hylerpeton, and Hylonomus were much more fully
known ; and it was a curious problem whether further research in
Europe would tend to reveal the existence during the Coal-period of
small Amphibia with well-ossified vertebree and well-developed limbs,
like the American forms, or whether it would show that the Labyrin-
thodonts of the European area rather adhered to the Archzegosaurian
type already known to occur in Europe, but not hitherto found in
America.

So far as the Irish discoveries have yet gone they prove the exist-
ence, during the Carboniferous epoch of Europe, of Amphibia which,
are analogous to, though altogether distinct from, the “‘ homotaxic ”
American Labyrinthodonts,—analogous to them in the degree of
ossification of the skeleton and development of the limbs,—different
from them not only in detail, but in the existence of such types as
Opluderpeton and Ichthyerpeton, which have at present no parallel
either in America or elsewhere.* |

The discoveries of the last five years show that the Labyrinthodont
Amphibia were as largely represented and as well developed in the
Carboniferous as in the Triassic formation. Three genera are known
from the Permian formation of Europe, and five from Asiatic, African,
and Australian rocks of an age which, if not certain, may safely be
assumed to be between the Carboniferous and Lower Mesozoic periods.

Professor Huxley concludes these observations by the following
remark :—* putting all these facts together, it would appear that
the Labyrinthodonts represent the first rope of the bridge which will
one day be suspended across the gulf which at present separates the
Palxozoic from the Mesozoic fauna.”

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxi

This interesting discovery in Ireland affords additional confirma-
tion of the correctness of the theory which assumes that new forms of
animal life, either as species, as genera, or as classes, were created or
made their appearance on our earth at the time when the conditions
of life were best suited to their existence, and that they were formed
with an organization adapted to the external conditions under which
they were to live. When we analyze the great Carboniferous de-
posits, and recognize in them the vast tracts of ancient swamps and
marshes covered with the rich and luxuriant vegetation which they
formerly presented, subject to the gentle oscillation by which they
were alternately submerged beneath the ocean and slightly raised
above the level of its waters, we find, as in the great dismal swamps
in some of the Southern States of North America, the very conditions
of life most suitable for reptilian existence ; and precisely on this;ho-
rizon they appear to have come into existence not in one or two vague
forms developed out of previously existing ones, but, as it is now
shown, in a great variety of new forms, all belonging to the same
reptilian class, varying in different hemispheres, but presenting
those peculiar characteristics which constituted them the fit inhabi-
tants of low swampy regions, clothed with an abundant yet varied
vegetation. Future discoveries will, no doubt, in time add to the list
of genera and to our more perfect knowledge of the reptilian fauna
of the Carboniferous age. In the mean time we may congratulate
ourselves on this great addition to our knowledge of this fauna, for
which we are indebted to the zeal and acumen of Professor Huxley
and Dr. Wright.

In the ‘ Bulletin de la Société Géologique de France’* will be
found an interesting account of the history of the discussion respect-
ing the Carboniferous formation of the Alps, by Prof. Alphonse Favre,
of Geneva, in which he describes the progress of the discussion which
so long prevailed respecting the age of the anthraxiferous formation
of the Alps, in consequence of the apparent intermixture or alternation
of beds containing vegetable impressions, supposed to indicate a
Carboniferous period, with beds containing Belemnites, supposed to be
of Jurassicage. You all, no doubt, remember the numerous memoirs
published on this subject, and of which a very full account was given
by M. Scipion Gras in a former volume of the ‘ Bulletin.’

M. Favre has taken up the subject, and has carried on the history
to the latest times. He divides it into four periods. I need not
trouble you here with any notice of the first two; and, with regard
to his third period, I will only observe, that it extends from 1858 to
1860, and contains an account of all the observations which tended to
prove the existence of the Triassic formation and of the Infralias, as
well as the consequences which resulted from this discovery. He
shows that the existence of these two formations created such a
break between the Lias and the Coal-formation, that it was no longer
possible to admit that the beds in question could belong to the same
age. The Trias was even discovered at Petit Coeur, so that this
locality could no longer be claimed as a proof of the union of the

® Qme sér, vol. xxii. p. 59,

lxii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Lias and the Coal-formation, and the battle-field of the discussion was
removed to St. Jean de Maurienne. The fourth period extends from
1860 to 1863. It began with the discovery of Nummulites at
Maurienne, and continued to the close of the discussion. Then it
was that the recognized presence of the Trias and the Infralias, as
well as the position of the Nummulites found in a formation hitherto
considered by M. Scipion Gras as anthraxiferous, combined with the
mineralogical character of the rocks, their stratigraphical position, so
long misunderstood owing to the numerous contortions of the beds,
and the fossils which they contained, proved the presence of the real
Carboniferous formation in the Alps.

The fact was generally admitted at the meeting of the French
Geological Society at St. Jean de Maurienne in 1861. The same
results were applied to Dauphiné and Provence ; and finally M. Heer,
who had so completely mastered the mystery of the fossil flora of
Switzerland, published in 1863 a memoir respecting the flora of the
Carboniferous formation in Switzerland and Savoy, in which he
showed that not one single plant of the Carboniferous formation of
the Alps was found either in the Lias or in the Trias.

Is it not a curious fact, observes M. Favre, that it required thirty-
five years of discussion and of argument to clear up a point of
Alpine geology? It has led, however, to a much better knowledge
of details; and now questions relating to the age of a formation
can be solved as well in the Alps as in the neighbouring countries,
and the charge of backwardness can no longer be maintained against
the geology of the Alps.

In concluding this précis, M. Favre gives a list of the various
geologists who had adopted the different views respecting the age of
the anthraxiferous: beds of Switzerland. In this list he places my
name amongst those who referred this formation to the Lias. Now,
although there can be no discredit in being placed in the same
category with such names as Elie de Beaumont, Sismonda, Collegno,
Roget, &c., I think it right to say that the only part I took in the
discussion was this, that in the anniversary address which I de-
livered from this chair in 1856, after giving a sketch of M. Scipion
Gras’s memoir on the subject, I stated, on the strength of the alleged
superiority of evidence derived from the fauna of a formation as to
its age, over that derived from its flora, that “ the weight of evidence
appears to be in favour of referring the whole formation to the
Jurassic rather than to the Carboniferous period.”

M. Favre also adds that, if the discussion had terminated in
the contrary sense, the whole question of paleontology would have
had to be seriously modified. If it had been proved that the coal
plants were still living during the Liassic period, the value of fossil
botany would have been destroyed, as it would no longer have served
to characterize a formation. The labours of Prof. Heer have saved
us from this catastrophe.

With reference to this question I may also direct your attention
to another memoir in the same number of the ‘Bulletin’ by M.
Lory, in which he endeavours to explain the stratigraphical anomaly

ANNIVERSARY ADDRESS OF THE PRESIDENT. lx

of Petit Coeur in the Tarantaise. The locality is a very limited one,
and the phenomena cannot be explained by inversion of the strata,
or by a turning over of the different beds. After describing the prin-
cipal facts, he shows that the anomalous position of these beds,
which had caused so much difference of opinion amongst geologists,
was owing to two faults, one general and the other local, and to the
slipping or sliding-in of overlying beds into the cavities thus caused,
and so bringing the Upper Lias beds in immediate contact with the
Coal-measures, and even the underlying crystalline rocks.

Neither time nor space would allow me to go through the numer-
ous works which the industry of the German geologists have pro-
duced on those portions of the secondary series, the Triassic and
Liassic formations, which are so extensively developed in the Alps
and in Germany itself. It would require volumes to do justice to
them all. I must therefore confine myself to a slight allusion to
some of the more interesting memoirs which have come under my
notice; and in doing this I feel it is impossible to withhold an
expression of admiration at the zeal and energy with which these
investigations have been pursued in so many different parts of Ger-
many. It is not that one eminent paleontologist has directed his
attention to this subject, but a whole army of eager and enthusiastic
explorers, animated by the recent rapid accumulation of facts, by
the discovery of new fossils, and by the greater accuracy with which
the different fossil-bearing strata have been distinguished, seem to
have come forth from every corner of Germany, each taking up some
special branch, and in the end almost overwhelming us with the
mass of accumulated results.

Professor Gumbel has published a very important memoir on the
‘geological conditions of the Triassic district of Franconia. After
describing the topographical features of the district under conside-
ration, he gives a general account of all its geological features,
showing that the crystalline rocks (Urgebirgs-felsarten) of the Oden-
wald form the basis of the whole system. The Silurian, Devonian,
and Carboniferous systems are wanting in this district. The con-
glomerates of the Dyas (Rothtodtliegendes) rest immediately on the
Urgebirge and form the basis of the Triassic formation (Bunter Sand-
stein, Muschelkalk, and Keuper), which fills up the whole region
between the crystalline rocks of the Odenwald and the Hercynian
mountain-system. It is well known that all the rocks of the Fran-
conian Alps rest upon this Triassic surface, and form a kind of insular
continent in the Keuper district.

The different beds and rocks throughout this region, with their
characteristic fossils, are then carefully described; after which the
author makes the following general remarks :—‘“ The long period of
time during which the massive rocks of the Jurassic formation were
gradually deposited in eastern Franconia, passed away without leav-
ing any additions to the rock-formations in the greater part of the
western district. Western Franconia was a continent of dry land
during this period of the formation of the earth’s crust. Not until
the Tertiary period did this district again share in those changes and

lxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

convulsions which were constantly going on—sometimes here and
sometimes there—over the whole surface of the earth. It is, how-
ever, comparatively only a small portion of the Franconian region
which took part in these changes during the Tertiary period; but the
new formations are of so gigantic a character that they make up in
intensity for what may be wanting in extent. To these phenomena
belong the volcanic formations, which were developed within the dis-
trict of the Rhon mountains ; they form a link in that great chain of
volcanic operations which connects the central mountains of Bohemia
through the Fichtelgebirge on the one hand, and through the Vogelsge-
birge and the Westerwald on the other, with the Siebengebirge.

Dr. Waagen has endeavoured in a short memoir to give us a general
classification of the beds of the Upper Jurassic formation, taking as
his basis the classification of English geologists, as the first which
was founded on a more accurate knowledge of the different beds,
although he doubts whether the names which were sufficiently
appropriate in the localities to which they were originally applied,
are equally so when applied to large areas where the same beds either
assume a different petrographical facies or are characterized by a
distinct or abnormal fauna. After describing the various local hori-
zons from the Portland Stone to the Oxford Clay, he endeayours to
establish a comparison between the English beds and those on the
continent, which are assumed to be their representative zones. The
following table shows how he groups these formations :—

Locat Horizons. Enexrisn Drvistons,
( Papi 1. Portland Stone.
| | Zone of Tregonia gibbosa .. 2. -Portlandisente

Region of S)

Se

Hexogyra virgula ......

eee

= ie |

S Orbicula latissima and

cb | Acanthoteuthis speciosa ..

® A er

re ; Region of

2 Ammonites mutabilis and »3. Kimmeridge Clay.
A

KS

Region of
Ammonites altcrnans and |
q Rhynchonella inconstans )

—

Region of 4, Upper Calcareous Grit.
|| Cidaris florigenmma ...... 5. Oxford Oolite.

(o) rs

ve
do) Region of ' .
& : Ammonites Martelli ...... } 6. Lower Cala a
Se ————

2
2) Region of

|| Ammonites biarmatus ....

\ 7. Oxford Clay.

ANNIVERSARY ADDRESS OF THE PRESIDENT. - Ixy

I must also notice the work of Dr. Ferdinand Stoliczka, entitled
“A Revision of the Gasteropoda of the Gosau beds in the Eastern
Alps.’ This memoir was written in Calcutta, where the author is
one of that band of geologists who, under the superintendence of
Prof. Oldham, are working out the geology of India. Having col-
lected in the Gosau district a vast amount of material before his
departure for the Hast Indies, he has been induced to publish his
observations in consequence of what he considers the great errors in
Herr Zekeli’s account of the Gosau Gasteropoda; and it was with a
view of rescuing geological science from these errors, some of which
are pointed out, that he undertook the critical examination of these
species, which have been too hastily increased in number by Zekeli
from 124 to 193 species.

With regard to this formation, I will only quote one sentence from
Dr. Stoliczka’s work, to show one facies of the Gosau deposit. “It
is well known that during some one of the elevations of the calca-
reous rocks of the Alps, after the deposition of the Lower Chalk, the
calcareous crust was cracked and opened out in numerous directions.
These fractures extended downwards to the ‘bunter Sandstein.’
The sea of the Upper Chalk period penetrated these openings, took
up its material chiefly from the ‘bunter Sandstein,’ and deposited
it again under a somewhat altered form. This is the reason why
our Gosau beds generally rest immediately on the ‘ bunter Sandstein,’
and why it is often no easy task to decide what is Gosau deposit and
what belongs to the ‘ bunter Sandstein.’ The occurrence of fossils
affords the easiest and safest solution of the question. The Gosau
beds were thus deposited in bays and inlets of the sea, which, how-
ever, had a far greater extension than now appears; not only the
abundance and variety of the fauna, but positive proof derived from
the conditions of the deposit leave no doubt on this pomt. Mighty
rivers soon emptied themselves into these bays, and drove away the
true marine fauna. A peculiar molluscous fauna developed itself at
the mouth of these rivers with species of Cerithium, Potamides,
Nerita, and Omphalia, accompanied no doubt by numerous fish and
gigantic Saurians.” He further shows that, under the influence of
this great addition of fresh water, the water itself became brackish,
or alternately marine and lacustrine. By degrees, the marine
fauna was checked and driven more towards the middle of the sea,
where it was powerfully developed in the neighbourhood of islands
or in other favourable localities.

I would also have given some account of the following papers, had
time permitted :—

“On the Cephalopod family Acanthoteuthis,” by Prof. Ed. Suess,
read at the meeting of the Imperial Academy of Sciences on March
16, 1865.

<©On the Formation of the Bunter Sandstein and Muschelkalk in
upper Silesia and its Fossils,” by Dr. Henry Eck.

«‘On the Tithonic Etage,” by Prof. Oppel of Munich, published
in the journal of the German Geological Society, 1865. This for-
mation.is intermediate between the Upper Jurassic and Lower Cre-

VOL, XXII. : e

Xvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

taceous beds, and the author defines it more strictly as occurring
between the Kimmeridge and lower Neocomian beds. It refers to
certain Alpine deposits containing Cephalopoda, probably corre-
sponding with Portland, Purbeck, and Wealden beds, but of which the
exact parallelism has not yet been sufficiently made out.

“On the Fauna of the St. Cassian beds, being a Supplement to the
Paleontology of the Trias of the Alps,” by Gustav Laube, in two
parts, the first of which contains a description of the Spongitaria,
Corals, Echinde, and Crinoide, with 10 plates; the second part —
contains the Brachiopoda and Bialves, also with 10 plates.

‘The position of the Raibl beds in the Franconian and Suabian
Keuper,” by Prof. F. Sandberger.

With reference to the much discussed question of the true position
of the Avicula-contorta beds, to which I alluded on a former occa-
sion, I find in the ‘ Bulletin de la Société Géologique de France,’
2nd ser. vol. xxi. p. 369, an interesting communication by M. Jules
Martin, entitled “The Rheetic formation or Avicula-contorta zone ;
its petrographical, stratigraphical, and paleontological constitution
in the different parts of Europe where it has been studied.” Dis-
satisfied with many of the results of previous investigations, M.
Martin determined to go fully into the whole question, the result
of which has since been published. In the meantime he here
gave a general résumé of what appeared to him the real state of the
case, after examining the data observed in different countries in
a mineralogical, stratigraphical, and paleontological point of view.

After describing the mineralogical character of the beds in question
in different parts of Europe, he comes to the conclusion that the
petrographical constitution of the zone is always dependent on the
nature of the underlying beds, or of the coasts which were washed
by the seas of this distant period. A coarse sandy conglomerate
when in contact with the crystalline rocks, becomes a fine sand
when it succeeds the grit of the Keuper, and marly limestone when
it rests upon the variegated marls and other argillaceous beds. Thus.
it often happens that the lower beds resemble, and even alternate -
with, the Keuper for a certain time, and then in the upper portion
pass by a regular transition into the overlying Lias. Mineralogically,
therefore, there is no evidence to show that it belongs to the Lias or
to the Keuper absolutely.

The same may be said respecting the stratigraphical evidence.
_ With the exception of a few local cases of a very limited character,
there does not appear to have been any violent or cataclysmal dis-
turbance, either at the beginning or at the end of the Avicula-con-
torta period. In general, these beds are found to be in a position of
conformable stratification, both with the Keuper and with the Lias.

The paleontological evidence is more important. M. Martin has
carefully examined all the lists given by the different authors who
have written on the subject, and endeavours to show how many
species and genera are common to the Keuper and the Avicula-con-
torta zone, how many are peculiar to this zone, and how many it
contains in common’ with-the overlying Lias. After eliminating

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxvii

useless synonyms, he proceeds to examine the geological limits now
known of the 149 genera, to which belong the 535 species which
form the fauna of this formation. He thus finds that only 12 of
these genera, containing 37 species, belong to the Paleozoic and Tri-
assic formations, and appear for the last time in this zone; that 47
other genera, comprising 71 species, appear here for the first time,
and extend in great numbers into the Jurassic series ; that some are
peculiar to this horizon, and that the remainder are common both to
the overlying and underlying beds. From these lists alone, we find
that the greater preponderance of forms connects this zone with the
Lias rather than with the Keuper. He then analyzes the different
classes with the same general result, except in the case of the Bra-
chiopods, which show a greater affinity to the Keuper than to the
Lias.

Again, looking at the question with regard to species, he finds a
far greater number identical with the Lias than with the Keuper,
and this with reference to the flora as well as to the fawna. The
next question is whether this zone is to be considered as a distinct
formation or merely as the lowest member of the Liassic series.
There can be no doubt, according to M. Martin, that the number of
organic forms which appear for the first time at this horizon is too
great and too important not to be considered as characteristic of a
distinct epoch; at the same time it is essentially Jurassic in its
character, and should therefore be considered as the lowest member
of the Jurassic series. The author concludes his paper with a series
of propositions involving in a concise manner the arguments above
recorded, but which it is hardly necessary to repeat on this occasion,
I will merely add that he gives a list of sixteen species common to
the Avicula-contorta zone and to the Trias, as well as another list of
fifty-seven species common to this zone and the Liassic formation.

Dr. Benecke, of Heidelberg, in his work on the “Trias and Jura
in the Southern Alps,” published during the present year at Munich
in the ‘ Geognostisch-palaontologische Beitriige,’ has taken another
view of this question, and endeavours to show, in opposition to the
views of Renevier,Stoppani,and others, that the Rheetic beds including
the Avicula-contorta zone, should be referred to the Trias rather than
to the Lias. He denies that the Infralias possesses that peculiar
character which justifies its being considered as a distinct formation
intermediate between the Trias and Lias. But, independently of this
question, the work of Dr. Benecke contains much valuable informa-
tion respecting the stratigraphical details of these formations, and
the comparison of those of Lombardy with those of Southern
Germany. Nor is the paleontological element overlooked. The
forms of animal life of the different strata are carefully compared,
and the whole argument is mainly based on sections which he has
himself observed in the different districts he describes.

On a former occasion I gave you some account of the observations
of M. Renevier on the Infralias or Rhetic beds in the neighbour-
hood of the Lake of Geneva. He has since published an account of
the geological formation of the Oldenhorn, a peak which rises to the

e2

lxvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

height of 3124 metres a little to the eastward of the Diablerets. A
short notice of this will not, I think, be uninteresting, as giving a
clear explanation of some of the complicated structures of the
secondary beds in this portion of the Alpine chain. After describing
the orographical limits of what he calls the massif of the Oldenhorn,
which is separated by a fault from the Col de Pillon on the north
or north-west, he describes the different formations of which the
northern slope of the mountain consists. These are broken into
several alternating anticlinal and synclinal masses, or,as he calls them,
combes and vallons, or saddles and troughs as they are sometimes
called. It forms a portion of the Cretaceous and Nummulitie zone of
the Alps. The principal nucleus of the formation is Neocomian, par-
tially covered over by the Urgonian limestone, resting on which are
occasionally found fragments of the Nummulitic beds, these generally
occur in the troughs formed by the synclinal arrangement of the
Urgonian limestone. Without going into all the details given by
the author, it may suffice to say that these beds, which are sometimes —
seen in an almost horizontal position, become, higher up the moun-
tain, completely vertical or even sometimes slightly inverted to-
wards the north. This alternation is repeated several times.

This remarkable arrangement, he observes, is precisely similar
to the saddles and troughs of the Jurassic chain, with this difference,
that the system of contortion which in the Jura has a horizontal
base, must be referred in the Alps to a highly inclined base line,
so that the two sides of a trough which in the Jura “ are symme-
trically inclined, become in the Alps the one horizontal, and the
other vertical.” This is well shown in his section of the Sanetsch,
where he has drawn an inclined ideal base line, which, when placed
in a horizontal position, reduces the Alpine contortions and inversions
_ to simple Jurassic undulations ; by this means the structure of the
Alpine beds is wonderfully simplified, and throws an interesting light
on the mode of elevation of the chain of the Alps. Here, at least, it
appears that the elevation of the Alps presents two principal elements.
The first action formed the undulations of the beds, producing a
structure analogous to that of the Jura; by the second, the whole
mountain-mass underwent an unequal amount of elevation starting
from the centre of the chain, producing an inverse effect on the un-
dulating beds, raising up and overturning some, while others were
brought into a horizontal position. This semi-jurassic orography
has given him the key to other stratigraphical arrangements in the
Alps, even more complicated and unusual.

The author then proceeds to describe the various formations, the
most recent of which is the Nummulitic, which consists of four dis-
tinct beds, and, as I have observed, always occurs in the troughs
formed by the synclinal Urgonian limestone. He mentions various
points where it is seen, and the different fossils by which it is cha-
racterized. Several species of Cerithtwm are abundant in the lowest
bed.

The next formation is the Urgonian. No traces of the Cerioma-
nian, Gault, Aptian, or Rhodanian have been here found. The Ur-

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxix

gonian formation consists chiefly of a white compact limestone. In
its fracture it is slightly crystalline, sometimes white, but more fre-
quently of a greyish hue, and except by its fossils is often hardly to
be distinguished from the Nummulitic limestone. Wherever the
Urgonian beds are broken through in the anticlinal saddles, a mass
of brown schists rises up below them. ‘The author attributes them
to the Neocomian formation on account of the fossils they con-
tain, as Belemnites pistiliformas, Blainv., B. dilatatus, Blainv., Ostrea
rectangularis, Rom., a-Hamite, and a Terebratula resembling T..
pseudojurensis, Leym ; at the same time he is not prepared to say
that other older beds may not also be associated with the Neocomian.

To the N. or N.W. of the Oldenhorn rises the Col de Pillon,
separated by a fault which follows the line of the river Dard to a
well known spot called Sur Pillon. The beds to the north of this fault
consist of alternating bands of gypsum and Corgneule or Rauchwacke,
which, in accordance with the views of Prof. A. Favre, the author
considers as belonging to the Triassic group. He has ‘traced them
to a considerable distance from the Plan des Isles to the eastward.
It is difficult to make out their stratification; M. Renevier suspects
that they represent repeated undulations of the same beds. They
are in part concealed under erratic deposits, and appear to be over-
lain by the sandstones, schists, and conglomerates of Palette du
Mont, the highest point of the mountain -mass to the north, and
which is laid down as F lysch. No fossils have been found in these
beds, nor in the gypsum or Corgneule of the Col de Pillon. The
latter is generally more or less cellular, and the gypsum varies from
‘white to grey.

Amongst the valuable works which have been published in Switzer-
land, I may also mention that of W. A. Ooster on the “ Pétrifications
remarquables des Alpes Suisses,’’ in which he gives a full synopsis
of all the fossil Echinoderms which have hitherto been discovered in
the Alps of Switzerland. The work is illustrated by twenty-nine
plates of fossils, and professes to give a description of all the species
hitherto known, from the Infraliassic beds upwards to the Tertiary
formations, amounting in the whole to 193 species, which are thus
distributed :—Trias 3, Infralias 4, Lias 4, Jurassic 27, Cretaceous
93, and Tertiary 62 species.

In the last year’s volume of the ‘ Zeitschrift der Deutschen Geolo-
gischen Gesellshaft’ will be found an interesting account of a visit
to the copper-mines of Monte Catini in Tuscany, and to some other
places in their neighbourhood, by Herr von Rath, of Bonn. The
mineralogical and physical features of the country are well pour-
trayed, as well as the different geological formations. The sterile
aspect of the Pliocene clay-hills, on which every attempt at culti-
vation has failed, is graphically described, and we have also a full
account of the Borax Lagoons (Lagoni) of Monte Cerboli.

There is, however, one passage in this memoir which has surprised
me. In describing the well-known statuary marble of Carrara, which
belongs to the Lias formation, the author says that in the Apuan Alps
the. finest statuary marble occurs in large lenticular masses, which

lxx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

are surrounded by a husk or crust containing much mica or tale and
other substances, and are imbedded in the common crystalline lime-
stone. This husk is called “ Madre-macchia ;” and the more it is
developed, the purer is the marble within. ;

This is precisely the manner in which the pure white alabaster of
Florence is found in the gypsum-quarries of Castellina, as I have
already described it*. I have also visited the marble-quarries of
Carrara but never observed this peculiar structure there. No doubt
the marble varies much in quality in different localities and on dif-
ferent hills, but it always occurs in large amorphous fissured masses,
all trace of stratification being removed by the metamorphism it has
undergone. If the author has not, as I suspect, confounded the
structure of the alabaster with that of the statuary-marble, it will
be a curious coincidence to find that both occur under such similar
circumstances. The explanation of this structure given by the author
is no doubt correct, viz., that during the metamorphosis of the lime-
stone or gypsum, the foreign particles mixed up with it were
driven out by chemical action and formed the Madre-macchia; and
the more this was done, the more perfect was the marble or ala-
baster.

Prof. Reuss has published in the ‘ Transactions of the Imperial —
Academy of Sciences at Vienna,’ a paper on a portion of the fauna
of the Upper Oligocene formation of Germany, viz. the Foramini-
fera, Anthozoa, and Bryozoa. The author’s former works on these
minute forms are well known; and, after alluding to the previous
partial publications of other authors, he observes that, owing to the
large mass of materials placed in his hands by numerous paleonto-
logists as the results of recent investigations, including all the
known German localities of Upper Oligocene beds, he has been
enabled to compile a complete view of the whole Foraminiferous,
Anthozoan, and Bryozoan fauna of the Upper Oligocene. Should
future researches lead to the discovery of a few more species, they
would only fill up gaps, but in no way effect any important change
in the general view of the question. Before describing the indivi-
dual species he makes the following remarks :—

1. Foraminifera.—Hitherto 142 species have been observed, with
two remarkable varieties. Of these only 5, which, moreover, are—
very scarce, belong to the division with siliceous shells; 16 species
have a thick calcareous shell without pores; the great majority,
viz., 121 species, have a calcareous poriferous shell.

From the table of genera it appears that the Rhabdoidez (with
21 species), the Cristellarideze (with 25 species), the Polymorphini-
dese (with 40 species), and the Rotalideze (with 19 species) are the
most abundant. The genera containing the greatest number of
species are, Cristellaria, Robulina, Globulina, Polymorphina, and
Rotalia. He then adds a list of those species which are the most
abundant and characteristic of the whole fauna, the more so as
they are almost all peculiar to the Upper Oligocene.

* Quart. Journ. Geol. Soe. vol. i. p. 282.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxi

He then arranges all the species in a tabular form, showing not
only their vertical range in the different Tertiary stages in which
they occur, but also their horizontal development, viz. the different
Upper Oligocene deposits in which they have hitherto been found.
This list shows that the Ahnegraben near Cassel has alone afforded
88 species, the greater part of aya are only found in few localities.
Very few species have a wide distribution. With regard to the
vertical distribution, 67 species have been found only in the Upper
Oligocene, to which they seem peculiarly to belong ; 47 species de-
scend into the Middle Oligocene or Septaria Clay, and of these 5
reach the Miocene, 3 the Pliocene, and 1 species is still living. Alto-
gether the Upper Oligocene has 42 species in common with the
Miocene, 5 of which extend into the Phocene and 10 are still living.

“ Taking all these facts into consideration,” observes Prof. Reuss,
“we come to this conclusion, that the Foraminiferous fauna of the
Upper Oligocene beds is very peculiar, and easily recognized under
all circumstances. The marks of distinction are partly common,
partly special: the former rest on the remarkable preponderance of
various Polymorphimdec and Cristellaridee, and on the abundance
of the otherwise scarce Flabelline; the latter on the numerous
species peculiar to the Cassel beds, amongst which the above-men-
tioned 17 species are remarkable, partly for the great abundance of
individuals, and partly for their distribution over almost all the
Upper Oligocene localities.”

The author then gives a description of all the observed species,
with their situation, history, and localities, and adds five well-exe-
cuted plates of figured illustrations.

2. Anthozoa.—Only seven species have hitherto been found which
can safely be referred to the Cassel beds; others may perhaps be
found by other authors, but the characteristic evidence is still incom-
plete. Of these 7 species, 3 belong to the Caryophyllidee, 3 to
the Turbinolie, and 1, viz. Cryptaais alloporoides, to the Madri-
poridew. Fragments of other species have, however, been found
too imperfect to describe, and authors have also quoted some which
Prof. Reuss has not had an opportunity of examining; the whole
number is therefore probably greater. The author then gives a
detailed account of the different species at present known to him.

3. Bryozoa.—These are much more numerous in the Cassel beds
alone. The author is already acquainted with 73 species, and there
are probably others. A tabular statement of their different locali-
ties then follows, from which it appears that they are very un-
equally distributed. Thirty-seven species have been found at Ast-
rupp and 28 at Luithorst. It is, however, worthy of notice, that
many of these Bryozoa extend through several stages of the Ter-
tiary formation, and they must therefore have continued to exist
through a long period of time. This is in direct.opposition to the
opinion of F. A. Romer, who has stated that each species of Bryozoa
is peculiar to one Tertiary formation, and that any one Bryozoon is
sufficient to fix the age of the formation in which it is found. This
Prof. Reuss considers to be an error. Then follows the detailed

lxxii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

account of the individual species. It must also be stated that the
work is accompanied by 15 plates of illustrations.

Although perhaps more interesting in an ethnological than in a
geological point of view, we cannot altogether exclude from our
notice the phenomena attending the first appearance of Man on our
planet. The discoveries of the last few years have satisfactorily
shown that the opinions formerly entertained of a great break
existing between the period when the now extinct races of Mam-
malia dwelt in our land, and the first creation of Man, are no longer
tenable. Here also we have been obliged to give up the theory of
great breaks between successive formations. As we find a gradual
passage from one geological formation to another evidenced by the
gradual dying out of the pre-existing forms of animal life, and the
gradual introduction of newer, and generally higher, forms (although
we do not yet understand the law of such progressive changes), so,
when we come to the most recent, or Quaternary, periods in geolo-
gical chronology, we find evidence of Man’s existence on the earth
before the final disappearance of those varied forms of mammalian
life which have hitherto been generally looked upon as belonging
to the final period of the geological cycle. Thus Man of the present
day is connected by an almost unbroken series of links with the
recently discovered Foraminifera of the Laurentian gneiss. Let me
not, however, be supposed to be thereby giving in my adhesion to
the doctrines of development, either to that of Lamarck or to the
more recent and captivating views of Mr. Darwin.

Since, then, we must now admit human remains, and the evi-
dences of Reman existence, as belonging to the last period of geolo-
gical history, I cannot refrain from alluding to some of the publica-
tions which have recently appeared on this subject.

Dr. Felix Garrigou, of Tarascon, has published an interesting
work on the old Quaternary alluviums and the bone-caves of the
Pyrenees and of the West of Europe. After pointing out that dif-
ferent caves contain different animal remains generally, in accord-
ance with the various positions of the caves, he shows that some
caves contain as many as three distinct beds characterized by their
different contents, as, ¢.g., the cave of Mas-d’ Azil.

The first period is characterized by Ursus speleus, U. priscus, .
Felis spelea, Hyena spelea, Hlephas primigenius, Rhinoceros ticho-
rhinus, Megaceros hibermcus, Cervus elaphus, Bos primigenius, Bison
europeus, and sometimes Cervus tarandus, &c. The second period
is that in which the Reindeer is most prominent; with it are found
the Horse, Megaceros hibernicus, Cervus elaphus, Bos primigenius,
Aurochs, Sheep, Chamois, Bouquetin, Wolf, and Fox, and a third
species of Canis, perhaps intermediate between these two last, but no
domesticated animals. The fauna of the third or prehistoric period,
found at.the entrance of caverns and in beds overlying those which
contain the Reindeer, consists of Ursus arctos (still living in the Pyre-
nees), three species of Bos (domesticated), the Goat, Sheep, Sus
scrofa palustris, Sus scrofa ferus, Cervus elaphus, Roebuck, Bouquetin,
Chamois, Wolf, Fox, domestic Dog, Hare, Blackcock, &c.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxiil

The author then observes that, “as the stratigraphical and pale-
ontological researches point to three distinct periods from the com-
mencement of the Quaternary epoch down to the historic times, so
the study of the remains of human industry, so constantly recurring
with the different faunas described above, also prove that these
divisions are correct ;” and he assumes that from the commencement
of the Quaternary epoch there are in the south of France three great
distinct phases in the palzontological history of this period, as well
as in the history of the civilization of the peoples which have lived
since the commencement of that epoch.

1. In the first great phase, Man was the cotemporary of the
ereat Cave Bear, and of all those animals which have been shown
as accompanying this great mammifer. The bones of these animals
lie together, broken by man, either in the old Quaternary alluviums of
the sub-Pyrenean valleys, in caves, situated from 150 to 250 metres
above the level of the present valleys. The remains of human in-
dustry found with the remains of these extinct mammifers indicate
an early art somewhat resembling that of the stone implements of
Abbeville.

2. During this first phase the great Carnivora and Pachydermata
became extinct. The Reindeer, owing to favourable conditions,
increased and multiplied, and became characteristic of a second
phase, during which Man had not yet learnt to domesticate animals.
But human industry had made considerable progress: the flints are
prepared with art and neatness, and bones are worked with more in-
telligence, as they show traces of sculpture and drawing. The Rein-
deer and its accompanying fauna are found in grottos situated near
the foot of the mountain, and at a lower level than those which con-
tain the Ursus speleus; they are also found in some caves in beds
overlying those which contain the mammifers of the older period.

3. The third phase is characterized by a fauna consisting chiefly
of domesticated animals, the remains of which are found at the
mouths of caves in the bottoms of the valleys, and sometimes in a
soil which forms beds overlying those containing either the great
Cave Bear or the Reindeer. Man has learnt to polish stones, they
are only occasionally cut; he is acquainted with agriculture, but
has not yet learnt the use of metals.

The author then applies these principles, with the same results, to
the other parts of France, as well as to Belgium and the west of Ger-
many, and concludes with a chronological review of the various
Mammalia composing the old Quaternary fauna, to serve as a basis
for the geological history of Man, which the author subdivides into
various epochs, from the doubtful Pliocene of Chartres to the earliest
historic period, and concludes with a sketch of some of the geolo-
gical causes which have led to the cave-phenomena of the Pyre-
nees, and a statement of the different heights at which these caves
occur, for which I must refer you to the work itself.

In continuation of his great work on ‘ Paléontologie Stratigra-
phique,’ M. d’Archiac has published another volume, entitled ‘ Le-
cons sur la faune Quaternaire,’ which the editor considers as a con-

lxxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

tinuation of the ‘ Introduction 4 l’étude de la Paléontologie Strati-
graphique,’ already published. It may also be considered as the
first application of the method recommended by him, and, strictly
speaking, as the commencement of his course of lectures, the object
of which is the exposition of the characters and of the distribution of
the fossil floras and faunas which have been successively developed
on the surface of the earth. In attempting to give a slight sketch
of this interesting work, I pass over the first lecture, which gives a
résumé of the first portion of his course. The second lecture describes
the Quaternary fauna of the eastern and central parts of France.
After alluding to the evidence of glacial action in the mountains of
the Vosges, the author states that the Quaternary deposits which fill
up the depression between these mountains and the parallel chain of
the Black Forest on the eastern border of the Rhine, consist of three
principal members.

1. The ancient alluvium, or loess, forms the uppermost or most
recent member.

2. Beneath this are beds of transported pebbles and blocks,
which, derived from the Vosges and the Black Forest, are connected
with the glacial phenomena of those chains.

_ 3. These again rest on a deposit of rolled pebbles, designated as
the Alpine erratic deposit, or Alpine diluvium, occupying the bottom
of the great valley of the Rhine.

These three deposits represent three successive epochs. The loess
is found on the flanks of the hills rising to a greater elevation in
proportion as we ascend the Rhine valley. At Bonn it is found at
an elevation of only 65 metres, between Heidelberg and Heilbron
at 260 metres, and on the flanks of the volcanic mountain of the
Kaiserstuhl it rises to the height of 400 to 450 metres. It contains
about 20 species of land and freshwater mollusca, most, if not all,
of which belong to living species. In its lower beds have been
found the bones of extinct Mammalia, Hlephas primigenius, Rhi-
noceros tichorhinus, Ox, Horse, and Deer. In the second deposit
have only been found a few species of freshwater shells, but in great
abundance. The third member or Alpine deposit is remarkable for
the great number of bones of extinct Mammalia found in it, in-
cluding, besides those just mentioned, Ursus speleus, Hyena spelea,
Cervus megaceros, Equus adamiticus, Bos priscus, and Cervus priscus.

He then compares the loess of the Rhine with the old alluvium of
the north of France; the second deposit is compared to certain por-
tions of the basin of the Seine, where beds of transported pebbles
and red sand without fossils are found ; and, lastly, the sands with
rolled pebbles forming the bottom of the plain of the Rhine are the
same as those which occupy the lower portions of the valleys of the
north of France and of Belgium, containing the same fossils and
offering the same physical characters, being exclusively composed
of the detritus of rocks which form the respective basins of each
depression.

Following this arrangement, the author describes the Quaternary
deposits of the different geological regions of France, giving full

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxv

historical details of their progressive discoveries and of their re-
spective authors. He then proceeds to discuss in the same way the
organic remains found in the caverns and osseous breccias in dif-
ferent parts of France.

In describing the caverns of Arcy near Vermenton in Burgundy,
he states that in 1858 M. de Vibraye undertook the careful exploration
and examination of one of these caverns. He made out the exist-
ence of three distinct layers or formations, and in the lowest, con-
taining the remains of Ursus speleus, Hycena speleea, Rhinoceros ticho-
rhinus, &e., he found a human jaw, still retaining two teeth zn situ,
in immediate contact with the bones of the extinct Mammalia. All
the characters of the substance of this jaw were identical with those
of the bones with which it was associated and very different from
those found in either of the overlying beds. With such evidence he
observes that it is almost impossible to resist the conclusion that
Man was the cotemporary of these extinct animals.

The author also shows, with reference to the caverns of other parts
of France, and especially in Languedoc and in the Pyrenees, that
incontestable evidence has been found, not only of the existence of
Man during the later periods when the Reindeer abounded all over
France and the great Mammalia appear to have become extinct, but
even during the period of their existence; and in concluding his
chapter on the caves and osseous breccias of the Pyrenees, he ob-
serves that, in the valleys of the basin of the Ariége alone, the
elements of human chronology from the earliest Quaternary epoch,
viz., that of the Ursus spelceus down to the time of the lacustrine habi-
tations of Switzerland, are such as have nowhere else been found
within so small a space; and he adds that, notwithstanding these
accumulated proofs, there are persons who still refuse to believe in
- the contemporaneity of Man with the great extinct species of Mam-
malia. <‘ But,” he adds, “ the history of science shows us at every
step instances of this opposition to the introduction of new ideas
contrary to old theories, and which wound the opinions and amour
propre of individuals ; let us not therefore be astonished at what we
see around us on this question, but let us hope everything from time
and perseverance in inquiries, which will ultimately get the better
of these oppositions as they have already done of so many others.”

The author then proceeds to examine these Quaternary deposits on
the northern and southern flanks of the Alps with the same general
results, those of the Mediterranean, Asia, North and South America,
Australia, and New Zealand, giving in every case an account of the
most recent discoveries bearing on this important and complicated
question ; and he shows, in conclusion, that the phenomena observed
in America and Australia confirm the observations made in Europe
and Asia, viz., that the fauna of the great extinct Mammalia cha-
racterized by the Elephas primigenius, Rhinoceros tichorhinus, Ursus
speleus, &c. must be separated from the fauna of the present day.
At the same time the difference between the characters of the Qua-
ternary fauna, when compared with those of the existing fauna, are
by no means the same in different classes: in the lower marine ani-

lxxvl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

mals, as well as in the land and freshwater mollusca, the differences
are very slight; amongst the mammifers it is generally the contrary.
The analogy of the Quaternary and modern faunas is subject to its
own particular law in each natural division; it is the more striking
in proportion as the animals under consideration are of smaller size.
If we examine the fossil Mammalia of the southern hemisphere,
either by orders, by families, or by genera, we first find that the
animals are larger than their congeners of the present day; and
secondly, that the species which are identical with those of the
‘present day, or nearly so, are the smallest.

After alluding to the theory of Prof. Owen in his Memoir on the
Megatherium, in which he endeavours to explain why the raées of
smaller forms of animals have had a more prolonged existence than
those of greater size, viz., because they could more easily accommodate
themselves to those changes in the conditions of life under which the
larger forms could no longer exist, he observes that, as a general
rule, we find in the different classes of fossil animals the duration
of species, and even of genera, is in an inverse ratio to their size and
mass, whereas the normal life of individuals is generally in a direct
ratio to their size.

“‘ It is,” he observes, in conclusion, “a mere question of time, for
which man, still new on the surface of the earth, has no chrono-
meter to enable him to measure the periods of existence of the beings
which surround him. Paleontology, it is true, reveals to us the
existence of gigantic reptiles in past ages, which have successively
appeared and disappeared; and the small animals, their cotemporaries,
have equally undergone the inevitable law of the renewal of types,
both large and small, and of their continual replacement. It is
true, we do not observe this movement about us; we are disposed
to believe that organic nature, which, since the beginning of crea-
tion, has never ceased to modify itself, has become immoveable since
Man’s appearance, that the laws of succession have been replaced
by mere laws of preservation; in a word, that creation is complete
and finished. '

‘«¢ This, undoubtedly, is an illusion, caused by this fact, that the
few dozen centuries which constitute our history are not sufficient
to bear witness to any important changes; but if study and observa-
tion have taught us anything, it is this, that the history of the whole
human race is of no more account in the history of nature than the
life of those ephemeral insects of which a single day beholds the
birth, the reproduction, and the death.”

An interesting Monograph has been lately published by Dr. G. A.
Maack, entitled ‘ Paleontological Inquiries respecting hitherto un-
known Lophiodon Fossils from Heidenheim on the Hahnenkamme
in Central Franconia, together with a Critical Review of all the
hitherto known species of the genus Lophiodon.’ In describing the
historical development of this genus, the author remarks that the
great gap which exists between the Ruminants and Multungula
(Vielhufer) of the existing fauna has been in a great measure
filled up by the discovery of fossil remains. The coxtrast hitherto

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxvil

supposed to exist between these different types has been removed
by means of the fossil remains of the now extinct Elasmotheria,
Palzotheria, Lophiodonta, Anthracotheria, &c. The object of this
memoir is to describe more fully than has yet been done the
peculiar zoological position of the genus Lophiodon, and its con-
nexion with, and difference from, allied genera, so far as it can be
done with the help of the hitherto discovered fossil remains.

He then proceeds to describe all the known species of Lophiodon,
and begins by subdividing the genus into the five following sub-
genera, according to the different structure of the teeth in each sepa-
rate species: —1. Coryphodon, Owen; 2. Tapirotherium, Blainy., this
is the typical form to which Cuvier gave the name of Lophiodon in
1822, although Blainville had already named it in 1817; 3. Pachy-
nolophus, Pomel.; 4. Lophiothervum, Gervais; and 5. Tapirulus,
Gervais.

The next subject to which the author directs his attention is the
examination of the Lophiodon remains of Heidenheim. This im-
portant discovery was made by Riitimeyer not long ago, and Dr.
Maack has been enabled to examine and compare about forty
well-preserved teeth, besides fragments of teeth, jaws, and bones.
These are all carefully described, and some curious anomalies in the
structure of the different teeth are pointed out. Thus he observes
that neither the molar nor premolar teeth of his new species, Z.
rhinocerodes, would, either in form or structure, give any clue as to
what the canine or incisor teeth were; on the contrary, we should
be greatly misled if we attempted, from the remarkable resemblance
between the molar teeth of Zapir and Lophiodon, to infer a similar
resemblance between the canine and incisor teeth of both animals.

He then discusses the zoological position of the genus Lophiodon,
and shows, as a necessary consequence of recent discoveries, and of
which he gives Rutimeyer the chief credit, that it belongs to the
great family of Pachydermata omnivora, and concludes that Lo-
phiodon is not connected with Tapir and Paleothervwm, although in
the structure of its teeth it combines many characters of these two
genera, but that it is more closely allied to the genera Cheropotamus,
Hyopotamus, and Anthracotherium.

With regard to the geological age of the beds in which Lophiodon
has been found, he comes to the conclusion, that this genus, with its
cotemporaries, formed a peculiar fauna, the remains of which are
buried in the clays, lignites, marls, freshwater conglomerates, and
marine limestones of the age of the calcaire grossier of Paris. The
work is illustrated by fourteen plates, chiefly representing the dif-
ferent teeth in various positions.

I think it may be interesting to allude here to a new theory
respecting the transport of erratic blocks recently published by
Count Keyserling*.

Finding great difficulty in accounting for many of the phenomena
which accompany the erratic blocks which cover the level lands of

* Mélanges physiques et chimiques tirés du Bulletin de Acad. Imp. des
Sciences de 8. Pétersburg, tome v.

Ixxvill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Livonia by the usually adopted theory of glaciers or of floating ice-
bergs, Count Keyserling calls attention to phenomena recently
observed on the shores of the gulf of Pernau as affording a more
satisfactory explanation, showing a movement of ice from the sea-
level inland and uphill.

During the first frosts of 1863, a vast field of ice, from 2 to 24
feet thick, had formed itself on the shore, extending far out to sea.
The water then rose about + feet, owing to the milder weather,
covering the field of ice. This was subsequently raised by the water,
and formed a free-floating field of ice of enormous extent. <A violent
storm on the 15th and 16th of January drove this field of ice against
the shore, and forced it with great power over the land. Similar
occurrences, but on a much smaller scale, had previously taken place ;
but now, owing to the much greater thickness of the ice, the event
assumed an intensity which had not been observed for several gene-
rations ; three peasants’ dwellings on the promontory of the Tackerort
were so suddenly invaded by the ice and destroyed, that the inhabit-
ants lost all their property, and had only time to escape with their
lives. The ice here rose 60 feet above the level of the sea; in other
places, where the shore was less steep and only 12 feet above the
sea, the ice came upon a fir-wood, broke the stems (some of which
were 13 inches in diameter), threw them down, and covered them
with an unbroken coat of ice. Wherever the floating field of ice
encountered a steep precipice, it rose up like a sheet of paper, its.
free edge rose over the land, and then, turning over, fell partly into
the sea and partly in fragments over the land and was pushed
further in. On the flat shore of Heuschliger the ice was driven
1023 feet inland, carrying with it a vast quantity of stones; at the
same time, stones were everywhere raised out of the sea by the ice
and driven on shore.

When Count Keyserling himself visited the spot, he found a block
of granite, weighing about 60 poods (2160 pounds), lying amongst the
blocks of ice, 30 feet above the level of the sea, and which had evi-
dently been raised by the ice from the bottom of the sea, thus con-
firming the generally received opinions respecting the transport of
stones by means of ice. In another spot, where there is a land-
cliff 30 feet high, he found a heap of ice-blocks 10 feet thick, which
had been generally tilted into an almost vertical position. Their
upper surfaces were covered with gravel and stones; the lower sur-
face was pure ice, and had originally formed the upper surface of
the field, thus showing that the broken masses of ice had been com-
pletely overturned by the violent pressure.

“Tf now,” adds Count Keyserling, ‘“‘ we could suppose that during
the period of the great erratic phenomena the same circumstance
took place, but on a larger scale, so that fields of ice of many hun-
dred square miles and 4 feet thick were periodically driven over the
land, we should have a natural explanation of the scratched sur-
faces in parallel lines, and also of the non-marine character of the
erratic deposits.” He considers that these phenomena show how
blocks of stone out of the sea can be pushed by ice into places far
beyond the reach of the water, and how deposits may be formed

ANNIVERSARY ADDRESS OF THE PRESIDENT. Lbe:00.4

along the coasts high above the level of the sea resembling true
inundations on the shore.

As an appendix to these observations of Count Keyserling, Prof.
Baer, of the Academy of Sciences, has added some interesting re-
marks of his own respecting huge boulders which he had himself
seen in various spots along the coast of Finland and the adjacent
islands, some of which are of great size, and all of which, he was
told by the inhabitants, had been driven into their present position
by the pressure of the great fields of ice. He then proceeds to give
an account of the island Laven Lari, on the coast of Esthonia, where
he considers that erratic phenomena are still going on, although the
chief events took place at a far distant period. He compares the
present form and outline, and its accumulation of gravels and boul-
ders, with those given in older maps, and believes that the map of
Spafariew, published in 1822, on data obtained in 1813, although
not absolutely correct, is yet sufficiently so as to justify the assumption
that the differences in the two maps represent the changes which
have taken place in the last quarter of a century. The reports of
the inhabitants respecting the movements of the ice would appear to
account for these changes, which are closely connected with the
facts communicated by Count Keyserling.

At the same time Prof. Baer admits that other causes of this
change of form may possibly have come into play ; as the inhabitants
alluded to the conviction of the gradual rising of their island above the
level of the sea, without, however, giving any satisfactory reasons.
In conclusion, Prof. Baer states, as the result of his observations, that
very large boulders are only seldom moved by ice; moderate sized
ones more frequently; but that small blocks, particularly near the
level of the sea, are so frequently moved and heaped together by ice,
that they escape the notice of the inhabitants, and yet produce im-
portant changes in the outlines of the flatter island in the course of
acentury. Thus erratic phenomena are continued even to the pre-
sent day, although the distribution of the superficial boulders appears
to point to an enormous lapse of time.

But there are other erratic blocks found buried in the soil far in-
land, which can hardly be referred to the action of the present sea
and its floating ice, and these extend as far as Moskow. In the Gulf
of Finland also are great masses of blocks which reach so near the
surface of the water as to cause serious impediments to navigation.
The Professor concludes by distinguishing still existing or recent
erratic phenomena from others which may be called diluvial, and
considers the floating ice and the present level of the sea, or perhaps
one slightly elevated, as a sufficient explanation of the former. With
regard to the older erratic or diluvial phenomena he has no suggestion
to make, but advocates the necessity of further local observations.

Don Casiano di Prado has published during the past year ‘A
Physical and Geological Description of the Province of Madrid.’ On
this occasion I need only refer to the second or geological portion of
the work. He says that in this province are found remains of the
organic life of the Silurian period in beds which rise to a height of

lxxx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

2000 métres, and this formation was not again submerged until about
the commencement of the Cretaceous period; but before the close
of this period both these formations were again raised above the sur-
face of the sea, and there is not the slightest evidence that they were
ever again submerged, as the Tertiary deposits which rest upon the
Cretaceous have been entirely, or at least for the most part, formed
at the bottom of a great freshwater lake. The Quaternary or dilu-
vial beds were also formed in fresh water, and at a period when
this lake had been partially filled up and drained.

The series of formations is therefore far from complete in the
province. Of the Paleozoic period, the Devonian, Carboniferous, and
Permian are wanting; of the Mesozoic or Secondary period there
are no traces of the Triassic, Jurassic, and a portion of the Cretaceous
beds; and of the Tertiary period only the Miocene occurs, there
being no certain evidence either of Eocene or Pliocene. The result
is, that the formations which are found in the province of Madrid
are Plutonic, consisting exclusively of granitic and gneissic rocks,
Silurian, a portion of the Cretaceous, part of the Tertiary, the Qua-
ternary, and recent formations.

The author then describes these different rocks, commencing with
the granite, which occurs principally in three distinct masses, lying
in a N.E. and 8.W. direction. But there are also numerous gra-
nitic islets in the gneissic rocks, many of which are so small that it
has been impossible to lay them down on a geological map; they
extend into the provinces of Toledo, Segovia, and Avila, and even
into those of Salamanca and Caceres, forming one of the most exten-
sive granitic regions of the peninsula. He then describes in great
detail all the different varieties of granite, passing into kaoline, syen-
ite, pegmatite, micaceous porphyry, and many others; also the ex-
ternal forms and structure of these masses, many of which are very
remarkable, caused chiefly by the unequal decomposition of the rock.
Isolated peaks and pillars, from 12 to 26 métres in height, have been-
thus produced, and the “ mountain of the seven peaks” has been
crowned with its seven isolated craggy rocks. These granite masses
are often traversed by fissures of various width, but sometimes large
enough to be used as threshing-floors by the peasants.

The author then enters into long details respecting the origin and
decomposition of the granite. He adopts the modern views that
water was no less necessary to its formation than fire, and thinks
that it must have formed the first crust of the earth, though he is
hardly prepared to say whether the granite of Madrid belongs to this
primordial granite, or to those masses which have been subsequently
erupted ; but there is no doubt that much of it belongs to the erupted
class. Some of the phenomena accompanying this process show that
not only have great disturbances and dislocations taken place, but
that the more recent and easily decomposed granites contain blocks of
an older period, and of a harder and more compact nature.

The gneiss is less extensively developed than the granite, but oc-
curs under a great variety of forms, as micaceous, felspathic, quartz-
ose, amphibolic, &c., all of which are described by the author; it

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxi

sometimes contains masses and veins of granite, in other places it is
interstratified with calcareous bands or nodules, metamorphic, and
so charged with magnesia as to be useless for burning. It is gene-
rally stratified, and rises into more rugged crests and crags than the
granite, though this is not so much the case in the province of
Madrid itself as in the neighbouring districts.

With regard to the origin of the gneissic rocks which were formed
by sedimentary action, the author observes that they are not all of
the same age. In the province of Madrid the gneiss is decidedly
metamorphic and contains beds of limestone which do not occur
in the Silurian formation. The gneiss has undergone much less
decomposition than the granite, although it appears to have been
eroded on a very large scale. This strikes Don Casiano as worthy
of notice, inasmuch as the granite contains 30 per cent. of quartz,
whereas in the gneiss this latter substance is almost entirely
wanting, and of the three component elements of both these rocks
the quartz is the least subject to decomposition. Other remarkable
instances of the decomposition of the gneiss are then described and
commented on; but my space and your time will not allow me to
enter further into their consideration.

The author then describes the Silurian formation, which, however,
is not of any great extent in this province; it consists chiefly of
slates, sandstone, and quartzite, the former being most preponderat-
ing. Roofing-slate does not occur here, though it is found in the
neighbouring provinces of Segovia and Guadalajara. The amount of
denudation in former periods has been very great, and the quartzites
which alternate with the slates having offered greater resistance to
this action are now seen standing out and forming rough and rugged
crests. After describing the principal strikes of these beds, which
oscillate from N. 20° E. to N. 22° W., and the metamorphic action to
which they have been exposed, the author proceeds to describe the
fossils which have been found in them.

These are very scarce in the province of Madrid, though many
casts of Giraptolites have been found in that of Segovia. Those de-
scribed here are :—Cruziana six species; Scolithus, Orthoceras, Lin-
gula, one each. Several forms of Acephala have also been met with,
but in too imperfect a condition to allow of their being satisfactorily
determined. ‘These’ are followed by an account of the veins and
minerals which occur in the granite, gneiss, and Silurian beds ; these
are both metalliferous and non-metalliferous. The latter consist
chiefly of pegmatite, quartz, and diorite: the metalliferous veins con-
tain a little silver, galena, sulphate of barytes, fluorspar, and iron
pyrites. These metals occur sometimes in detached masses or no-
dules, and sometimes disseminated throughout the whole substance
of the rock. Between the years 1841 and 1860 there was a great
development of mining enterprise, but the results were anything
but satisfactory.

The author then describes in detail the various minerals found in
the granitic, gneissic, and Silurian rocks, and concludes this portion
of his work with an account of the different systems of elevation

VOL. XXII.

Ixxxii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

which prevail throughout these formations. The direction of the
principal mountain-chain which traverses the peninsula from Lisbon
to the Pico de Grado, passing through the provinces of Segovia,
Soria, and Guadalajara, is from E. 27° N. to W. 27° S.; four other
important mountain-chains run nearly parallel to it, although slightly
obliquely. The author then, taking up the views of M. Elie de
Beaumont, endeavours, I think somewhat hastily, to refer these dif-
ferent lines of elevations to the different systems laid down by the
great French geologist in the European region: thus he refers the
chains of the Guadarama, La Gata, and La Estrella, the mean direc-
tion of which is E. 39° N., to the System of Westmoreland, which
throughout Europe oscillates between N.E. and E.N.E. But it is
unnecessary to pursue this question any further.

Cretaceous formation.—In the district under consideration Don
Casiano has found only one of the four groups into which M.
d’ Archiac divides this formation, namely, the Lower Chalk (crace tuf-
feau), the second in descending order. He has found no trace either
of the white chalk immediately above, or of the gault immediately
below, or of the fourth or lower group. It is found only in narrow
and contorted bands in certain spots; this is all that remains of
the greater extent of ground it must have originally covered, except
such portions as may be concealed by the Tertiary and Quaternary
deposits, and which towards the south may extend continuously into
the province of Cuenca. There is no appearance that the Cretaceous
sea ever extended further west than the Mota del Cuervo in this
. last-mentioned province, orQuintanar de la Orden in that of Toledo,
or Quijorna in that of Madrid, Espinar in that of Segovia, or the
river Luna in the province of Leon. In this ancient sea the Sierra,
or mountain-chain of Guadarama, formed one peninsula, which termi-
nated towards the east, not far from the Pico de Grado, and another
smaller, within the province of Madrid. The author then describes
the different bands which he has examined; their dip is generally.
8.E., and they are of no very great breadth or length, but are natu-
rally broader where the dip is less. One of these bands, in the -
neighbourhood of Atalaya del Vellon, has been broken through at
the spot where its strike is curved / ‘round, forming a gorge of a few
metres in breadth, at the bottom of which the mica schist (mzcacita)
on which the chalk rests is exposed.

The prevailing rock in this formation is limestone, varying much
both in colour and in structure,.being occasionally quite spathose or
crystalline ; very little of it, can be used either for building-pur-
poses or for lime. It is sometimes argillaceous or marly. Chalk-
marl occurs in some of the beds, as well as sandstones, apparently
Greensand. In this and in the ‘lower beds a few traces of lignite
oceur, which in former times, and especially in the reign of Charles
III., gave rise to the most extravagant expectations respecting the
coal of Manzanares, which was said to be superior to that of En-
gland, because it contained more sulphur! The greatest thickness of ©
the Cretaceous formation is about 300 metres, but in many places it
has been reduced by denudation to from 20 to 25 and even 17 metres.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxxxiil |

A description of one section given by the author as seen between
Madrid and Burgos, before entering Molar, will suffice to give an
idea of the superposition of the beds. They dip 30°8.E. The base
consists of a few metres of arenaceous beds resting on the gneiss,
having in the middle a thin band of limestone. These are followed
in ascending order by a considerable thickness of limestones of
various qualities, succeeded by a thick mass of marls and argilla-
ceous limestone, and thin beds of limestone containing an irregular
tabular vein of manganese ; the whole being followed by the dilu-
vial gravels. In some places, as at Atalaya del Vellon, marly beds
are interstratified with the lower arenaceous beds. After describing
the general form-and structure of the principal masses of this for-
mation, which has a general inclination of from 20° to 50° to the E.,
N.E., and 8.E., according to the great bend to which these beds have
been subjected, circling as it were round a central point, the author
notices the principal escarpments and ravines, and some of the
numerous and extensive caverns met with in this province.

He then proceeds to describe the fossils of the formation.
These are very few, but, as he observes, sufficient to identify this
formation as the second group or Lower Chalk. The following are
the species found and described by Don Casiano :—Astarte striata
Sow.; Arca Cenomanensis, VOrb.; Mytilus Vernewh, a new species
resembling M. alternatus; Lima cretosa, Duj.; Lama dichotoma,
Reuss ; Avicula pectinoides, Reuss ; Avicula Villanovana, a new spe-
cies; Pecten tricostatus, Bayle; P. quinquecostatus, Sow. ; Spheru-
lites squamosus, d Orb. ; Hemiaster Fourneti, Desh. ; Nucleolrtes lacu-
nosus (?), Agas., in bad condition ; Arca, new species, resembling -A.
Taalleburguensis ; Terebratula, probably a new species. The author
also mentions other genera, of which he discovered fragments too
imperfect to enable him to give their specific denomination, as a
claw of a Crab, the cast of a Trlostoma, three species of Cardium, a
Cardita, Cyprina, Arca, Mytilus, Modiola, two species of Ostrea,
several Rudistes, and two small Echinodermata.

It may be here observed that the general facies of this list, im-
perfect as it is, corresponds with the fact mentioned by Sir C. Lyell in
the last edition of ‘The Elements of Geology’*, that in the rocks of
the Cretaceous era in the south of Europe Ammonites are scarcely
ever found, and the genera Hamites, Turrilites, Scaphites, and perhaps
Belemnites, are entirely wanting ; while, on the other hand, genera
belonging to the great family of the Rudistes of Lamarck are gene-
rally abundant.

Tertiary formation.—This forms one of the three great belts into
which the province of Madrid is divided, both geologically and geo-
graphically, extending from N.W. to S.E. Its thickness is consider-
able, but, owing to the effects of denudation, it is very variable ;
in some places, however, it is known to attain a thickness of about
340 metres without reaching the base. It is not a marine forma-
tion. The only fossils hitherto found are of terrestrial or freshwater

% ‘Hlements of Geology,’ by Sir C. Lyell, 6th edit. p. 334.

n>

Ixxxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

origin, and they appear to belong to the Miocene period; conse-
quently there was here a vast freshwater lake, extending from the
Sierra de Guadarama to the Sierra Morena and Montes de Toledo,
and even to the mountains of Valencia and Murcia, although in this
direction it is somewhat difficult to fix its limits. The rocks of
which it consists are limestones of different varieties, clay, gypsum,
marls, sands and gravels, siliceous beds (pedernal flint), magnesite,
and conglomerate or pudding-stone; the three former are the most
abundant, and they are not associated with any plutonic or volcanic
rock in the province. A considerable portion of the upper bed has
been removed by denudation; by this means, and owing to the
violent action of the rivers during the Quaternary period, the physical
aspect of the country has been greatly modified. Low plains and
narrow valleys have been formed, which haye been again partially
covered up by diluvium. In other places where the beds, which are
generally horizontal, have not been affected by denudation, they
form vast upland plains, called wildernesses or deserts (pdramos) ;
but where the upper bed of limestone has been removed by denuda-
tion the surface is much more irregular. Generally speaking, the
structure or arrangement of this formation is simple enough where
the strata are horizontal; but this is not generally the case, as the
author proceeds to show in detail, and particularly in some places
where the inclination of the strata is almost vertical.

This formation may be separated into three divisions. Limestone
prevails in the upper almost exclusively ; the middle division, which
has the least thickness, consists chiefly of clay and gypsum, and the
lowest consists of sandstones and conglomerates. The author then
describes in great detail various localities where these different beds
are found alternating with each other, and varying even within
short distances, the chief peculiarity being that the gypsum always
occurs in the central beds. The best building-stone in the province
is quarried in the neighbourhood of Colmenar de Oreja ; the quarry-
men give a different name to each band. Some are better than
others; but all are rather apt to split, and great care is necessary
in using them for building-purposes to see that the blocks are placed
in their natural position.

_ The siliceous deposits are the most irregular in the whole forma-
tion. Sometimes the silex forms large masses in the clay; some-
times it occurs as small angular blocks. Near Vicdlbaro rounded
blocks of the same substance are found, and in one spot large irre-
gular nodules or slabs of flint form in the clay an irregular bed,
which is extensively quarried and used in Madrid.

In order to account for the great variations which occur in these
beds even within short distances, the author refers to a suggestion
thrown out by M. d’Archiac, namely, that the material for these rocks
was supplied from copious mineral springs, and is not alone the result
of matter transported by the streams from the surrounding hills.
But this explanation does not appear to him sufficient, even without
taking into account those rocks which could not have been formed
in this manner ; and he observes that this variation is the more re-

ANNIVERSARY ADDRESS OF THE PRESIDENT. ]xxxv

markable, inasmuch as it does not occur in the older rocks, which
are generally persistent for great distances and throughout their
whole thickness, except in the case of the conglomerates.

Amongst the special phenomena which the author describes in
this formation, may be mentioned the great inclination of the upper
limestone beds in certain localities, also that the disturbances in
the stratification of the zone of clays and gypsum are much more
distinct than in the upper zone of limestone ; they present nume-
rous undulations more or less abrupt in their stratification. On the
left bank of the Jarama are the soda-mines of Protectora, 4 or 5
kilometres east of Crempozuelos; the beds are horizontal and con-
sist of clays and gypsum. The sulphates of soda and of soda and
lime which are worked, occur chiefly in the clays extending through
a thickness of about 15 metres; they occur either in detached
masses in cracks and hollows, or disseminated throughout the whole
mass. One of these cracks is very remarkable, having an undulating
course in a more or less horizontal direction. Other local distur-
bances and unconformabilities of the different strata are described;
they are probably owing to some agitation of the waters of the lake
during the process of deposition. The origin of these rocks is
attributed to mechanical or chemical causes, and sometimes to a
combination of the two. The origin of the gypsum appears to the
author more involved in difficulty. Was it derived from springs of
water which held it in solution, or was it the result of metamorphic
action? The gypsum of Madrid is found in beds and in the crys-
talline form of selenite. Masses of both kinds occur also in the
argillaceous beds; sometimes only loose plates of selenite occur, at
others it occurs in veins either single or intersecting each other, and
in many other forms. The saccharoid gypsum or alabaster is scarce
in this province, but it abounds in the neighbouring province of Gua-
dalaj ara, where it forms large masses or nodules, which are enveloped
in a red argillaceous covering or coat*.

The formation of silex and resinite was also probably owing to
springs containing it in solution. The emission of silex during this
period must have “been enormous, for almost all the Tertiary lime-
stones contain it in large proportions, as much as 20, 30, or 40 per
cent. Magnesia and salts of soda are also abundant ; but rock-salt
does not exist in this province, although it is found in the neigh-
bouring province of Toledo, on the south side of the Tagus, and in
the district of the Ebro at Remolinos, province of Zaragoza. Here
the beds of rock-salt are of great thickness, it being, as the author
observes, a remarkable fact that this substance, originally derived
from the sea (?), should oceur so aay in a freshwater forma-
tion.
The author next describes in detail the different minerals found
in this formation, many of which are interesting, and might be made
of great commercial importance ; they are quartz, flint or'silex, resi-
nite (both opal and hyalite), nitre, salt, sulphate of soda, thenardite,
_ * See Description of Nodules of Alabaster in the Mines of Castellana i in Tus-
_cany, by W.J.H. Quart. Journ. Geol. Soc. vol. i. p. 282.

lxxxvl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

glauberite, carbonate of lime, sulphate of lime, magnesite, argile, and
traces of lignite. With regard to its paleontology, the author states
that, strange as it may appear, not a single fossil shell has been
found of which it was possible to determine the species: the fos-
sils belong to the genera Hehw, Lymnea, Planorbis, and Paludina.
Melanopsis has been found in the neighbouring provinces of Guada-
lajara and Toledo. This is an interesting fact, inasmuch as Spain is
the only European region in which a true living Melanopsis is found,
if we except M. buceinoides or prerosa, which is found in Greece,
but belongs to the Asiatic provinces, being abundant in many, parts
of Asia Minor.

With regard to the land and freshwater shells of this ieee for-
mation, the author observes that he has only found casts of them ;
and after pointing out the importance of local monographs of differ-
ent Tertiary districts in Spain, he observes that, “if a geologist
would devote himself for several years exclusively to the study of
the Tertiary formations of the peninsula, he has no doubt but that he
would discover numerous fossils of many classes.”

Mammalian remains, however, have been found in a better state
of preservation, and these are decidedly characteristic of the Miocene
age. No bones have been found in the upper or limestone zone in
this province; but they occur in the underlying marls and in the ~
neighbouring province of Toledo, near Barcience. The characteristic
species which the author has met with are Mastodon angustidens,
M. taprroides, Palcotherium Aurelianense, and Hipparion, and a
questionable case of Anoplotherium murinum. For better identifiea-
tion the author has added engravings of most of the dental remains
which he found; and in addition to those mentioned above is a molar
tooth of Rhinoceros Matritensis, Lartet, a molar of Sus, probably S.
Lockart.. Sus paleeochwrus has also been found near Madrid, but
the author had not seen it, as well as molars of Palwomerya, pro-
bably P. Bojani.

The author then describes the different elevatory actions to which
the Cretaceous and Tertiary formations have been subjected. These
have evidently been both partial and general; but, as the author
observes, much remains to be done, in Spain particularly, to enable
the geologist to reduce the elevatory phenomena to anything ap-
proaching a perfect system. ‘The concluding portion of the work is
devoted to a minute examination and description of the deposits of
the Quaternary or Diluvial period; the various phenomena attend-
ing them and the different rocks of which they are composed are
analyzed with great care. Traces of glacial action are uncertain ;
the author rather inclines to the belief that the Diluvial beds owe
their origin to aqueous causes; a certain amount of stratification is
generally visible. The Diluvium may be separated into three diyi-
sions; the uppermost, which is most seen in this province, consists
of sands, the second of marls and clay, and the third or lowest of
gravel or stone. These are the terms usually applied by the workmen;
but, as the author observes, there are clays and gravel in the upper-
most, gravel and sand in the second, and sand in the lowest beds. He

_ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxxvil

then describes the successive changes and phenomena which took
place during this period, tending to the deposition and formation of
the different beds; he also alludes to the great changes which the
older rocks themselves, which form the Diluvium, have undergone
during this period. The quartz and quartzites are generally only
changed into rolled pebbles, although some blocks of quartzite
are to be seen with traces of a conical structure, as if they had
been violently struck with a heavy blow; this is shown on the out-
side by circular fissures which penetrate into the interior, expand-
ing more and more from the centre ; the feldspar and Silurian slates
are reduced to an argillaceous state. Even the blocks of granite
have so completely lost their coherence that they can be cut through
with the spade or mattock. The same thing occurs with the lime-
stone, and even with gneiss, which is generally so little liable to de-
composition. One of the most remarkable diluvial phenomena in
this district is, that the calcareous rocks, after losing their coherence
by the operation of diluvial agents, and being scattered amongst the
sands and clays, did not become mixed up with them, but remained
quite isolated, although reduced to a soft earthy state. Very few
eases of hard rock occur in the Quaternary beds, although the author
observed a few small bands or patches of conglomerate or pudding-
stone cemented together by a calcareous or ferruginous matrix.
Calcareous tuff is very scarce. There are very few caverns of any
importance in the limestone rocks in this district. There is only
one worth noticing, called the Cueva del Reguerillo, in the Ponton
de la Oliva; it contains numerous stalactitic and stalagmitic forma-
tions. No bones, ancient or modern, have been found in it; but as
yet no excavations have been made in the stalagmitic bottom, al-
though in the neighbouring provinces of Segovia and Guadalajara
there are several caverns from which objects of great interest have
been collected. The author does not say what they were.

The paleontological discoveries in this Quaternary formation are
extremely poor in Spain, in the province of Madrid almost nil;
tusks and bones of an elephant were found by M. Graells near San
Isidro. This probably belongs to a new species; for the author states
that Dr. Falconer, who saw the remains in Madrid, at once declared
that they did not belong to either Elephas primigenius, or E. afri-
canus, or H.armenianus. Another lower jaw with three molar teeth,
also found near-San Isidro, probably belongs to Cervus elaphus.
Cervus tarandus has not yet been found in Spain, and it is remarkable
that these two species are never found inhabiting the same locality.
. The author concludes with an account of some flint hatchets found
in the diluvium of San Isidro, as far back as 1850, in the gravel and
below the beds containing the elephant bones, and with some re-
marks on the antiquity of man, on the recent and vegetable soils,
and on the remains of pre-historic times. He feelingly alludes to
the difficulties he has had toe contend with in the total absence of all
geological observations on this district before he undertook his task ;
and every geologist will sympathize with his last words—“ I always
started from Madrid with my knapsack and hammer cheerful and

IxxxVlil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

full of joy, on my return I never entered its gates without a vague
feeling of sadness.”

I have much pleasure in stale that four more parts of the work
of Major Crescenzo Montagna, entitled ‘Generazione della terra,’
to which I alluded on a former occasion, have since been published ;
they are written in the same moderate and careful spirit as the
former ones. The author has avoided all extreme and exaggerated
views. He adheres to the generally received opinions respecting the
fixity of species, and protests strongly against the doctrine of trans-
mutation and the Darwinian theory. In the 16th and 17th
chapters of the fourth book will be found some interesting consider-
ations respecting the appearance and disappearance of species on
the surface of the earth. He rejects the doctrine of great breaks in
the order of succession of animal life, as well as of those cataclysmal
paroxysms which are supposed to have caused them; on the con-
trary, he finds a passage of genera, and even of species, from one
formation to another; many species have survived the causes which
led to the destruction of others, and have continued to live on
together with the newly created forms. And with regard to the
introduction of new and the extinction of old species, he points to
many causes which may have occasioned the latter phenomena; but
he maintains that man in his present state of knowledge is unable
to understand how new forms have been brought into existence,
except by the will and law of the Creator. With regard to the ex-
tinction of species he has, however, committed one serious geogra-
phical error when he states (p. 335), “ Quite recently, according to
Lyell, the extinction of the Dodo has been noticed, a bird which at
no very distant period was an inhabitant of the British Isles.”

He protests in the strongest language against the doctrine of
transformation of species, and considers the idea that a mollusk could
become a fish, or a lizard a man, as worthy only of a madman, and as
giving but poor evidence of the progress of civilization at the present
time.

In a subsequent passage, however, he bears testimony to Mr. Dar-
win’s great merits in showing to what an extent the variety of species
does sometimes extend, and in endeavouring to get rid of the endless
multiplication of species which some naturalists endeavour to set up
on the strength of slight variations of form and markings, which are
really only the result “of local conditions or a change of geographi-
cal position.

The work is accompanied by numerous plates, drawn and engraved
by the author himself. It is, however, to be regretted that the work
has not been more expeditiously completed, as the last numbers
have not yet been published.

In the Bulletin of the Geological Society of France for last year*,
M. Boué has published a paper giving his reasons for now modifying
some of his views respecting his classification of Turkish Geology,
published in 1840. Human knowledge, he says, advances by the ©

* Bull. de la Soc. Géol. de France, dewxieme série, vol. xxii. p. 164.

ANNIVERSARY ADDRESS OF THE PRESIDENT. )xxxix

discovery of new facts as well as by the application of new theories.
He shows that this has been the case in every branch of science.
Zoology, propped up by comparative anatomy, is now a very dif-
ferent science from what it was; it is the same in the case of geo-
logy, both theoretical and practical. About 20,000 works or me-
moirs have as yet appeared on geological geography, the publication
of which, during the last fifty years, shows a kind of geometrical pro-
gression. The range of geological science increases in proportion as
we discover new facts, and these again increase the number of for-
. mations and the limits of their successive beds.

M. Boué then points out the difficulties he had to contend
with when he made his expeditions into Turkey, partly owing to the
social and physical condition of the country itself, and partly to the
total absence of all knowledge respecting the phy sical features of the
country and the want of correct maps. Even the geology of the
neighbouring countries with which that of Turkey in Europe is con-
nected, namely, the Eastern Alps, the Carpathians, and Transylvania,
was but imperfectly known at that time. Thanks to the Geological
Institute of Vienna, these points have now been clearly made out,
and we have the means of instituting a more satisfactory comparison
between the formations of the two districts; but a new expedition
into Turkey in Europe is much wanted. In the meantime, M. Boué
endeavours in the following propositions to point out some of the
errors contained in his former works :—

1. He is convinced of the existence of the Palwozore system in
Turkey in Europe, not only along the Bosphorus and in the central
portion of the chain which runs along the coast of the Black Sea, the
Little Balkan, but also in the centre of Upper Meesia, and in the
middle of Bosnia, about Voinitza, towards Trawnik and Kiseliak.

2. If the old Carboniferous formation appears to be wanting in
Turkey, the Zrias of the Alps and the Carpathians, with its peculiar
facies, exists in many places, as in the south-east of Servia, in
Western Bulgaria and Upper Mesia (part of Servia), and in parts of
Bosnia. He does not believe it exists in Epirus or Albania. It is
probably covered up by younger formations in the Herzegovina. M.
Hauer has found a trace of it at the southern extremity of Austrian
Albania.

3. The Alpine Lias, that compact and pacts dolomitized limestone
characterized by Megalodon, appears to occupy a considerable portion

_of Turkey, particularly in Bosnia and Servia, and many other locali-
ties which are mentioned by the author with more or less cer-
tainty.

4, Various Jurassic beds, which, for want of evidence, cannot be
more specially described, occur in the mountains of the Bannat and

eServia, and in the south-west of Servia, in Bosnia, and in Mount
Pindus, now Mezzovo, and in the chain of Agropotamos [query As-
propotamos?]. He also is of opinion that the beds of Késsen and of
Hierlatz occur in Bosnia.

5. The Dolomitic formation forms a serrated and sometimes double
ridge between the Prokletia and the Albanian Drino as far as Vronatz

xe PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

in Central Bosnia, as well as in the south of Montenegro, in Mace-
donia, and in other places. He thinks it was a mistake to class these
rocks with the Cretaceous system, on account of their close resem-
blance to the dolomites of the Tyrol and of the Eastern Alps. He is
inclined to adopt the view of M. Richtofer, that the dolomites are
the remains of coral-reefs partly denuded and considerably mine-
ralized.

6. The Neocomzan system appears to be very abundant in Turkey
particularly in the Balkan, Upper Eastern Macedonia, Western Dar-
dania, and in Servia, probably also in Bosnia. It is very fossili-
ferous.

7. The Cretaceous formation with Orbitolites traverses the whole
of Bulgaria a short distance to the north of the Balkan. It also oc-
curs in the centre of Servia, with many fossils.

8. The Gosaw formation is found occasionally in Turkey, parti-
cularly in Eastern Servia and in Bosnia, characterized by Tornatella
gigantea. Limestones with Nerinea are also found in Upper Al-
bania.

9, The Cretaceous system with Rudistes occurs in considerable
masses throughout Western Turkey and in Macedonia, as well as in
Servia. It is marked by bands of fossils on several plateaux of the
limestone-mountains of Bosnia, Upper Albania, and Mount Pindus,
as well as in the south-west of Macedonia. |

10. The Chalk-marl with Belemnites has only been observed in
Western Bulgaria.

11. The Eocene arenaceous beds of the Carpathians and Vienna, or
the Tertiary flysch, is well developed in Central Servia, Western Bul-
garia, Epirus, and Southern Albania along the coast.

12. The Nummulitic system occurs in parts of Albania towards
Epirus, in the west of Thessaly, Southern Albania, and in the Her-
zegovina, as well as in the neighbourhood of Varma, in Bulgaria, and
in Eastern Thrace.

13. The Miocene formation, or rather the Neogene of Vienna, is
found with its clays and fossiliferous limestones in the great Servian
valleys, in the basins of the Nish and Upper Drin, and in numerous
other basins throughout the country.

14. Erratic blocks are doubtful.

15. The author also mentions several places where the Eocene beds
have been pierced. by serpentines, diorites, and metalliferous por-
phyries.

In the ‘ Smithsonian Contributions to Knowledge’ for 1865 will be
found an interesting work by Dr. Leidy on the Cretaceous Reptiles of
North America. The author had originally intended to include an
account of the fossil fishes, and thus to form a monograph of the ex-
tinct vertebrata of the Cretaceous period; but this he found was
impracticable at present. No other vertebrata, birds or mammals, have
been found in the Cretaceous deposits of any part of America. Most
of the fossil remains described in his memoir were obtained in New
Jersey ; many were found in the Greensand, which is largely exca-
vated for agricultural purposes, and others were obtained from lime-

ANNIVERSARY ADDRESS OF THE PRESIDENT. xc

stone beds. The Cretaceous formations constitute a large tract of
country, extending through the States of New Jersey, Maryland, and
Delaware ; they appear in isolated patches in North and South Caro-
lina and in Georgia. More extensively developed in the western
portion of the latter state, they curve in a wide crescent-shaped tract
‘through Alabama, Mississippi, and Tennessee, to the mouth of the
Ohio river. Thence, passing in a narrow band through Arkan-
sas, they afterwards expand to an enormous extent, and occupy a
great portion of the region between the Mississippi river and the
Rocky Mountains, reaching north into the British possessions and
south into Mexico.

Then follows a very detailed account of all the species hitherto
found in the United States, the most characteristic of the Crocodilian
remains being a nearly entire skull of Thoracosaurus neocesariensis.
The species described are 28 in number, belonging to 23 genera, viz.
18 Saurians and 5 Chelonians. The work is illustrated by 20
beautifully executed lithographic plates, and the author anticipates
that, when the western and southern Cretaceous regions shall have

been explored, many additions will be made to these remains, nearly
all of which have been obtained from the eastern border.

I stated last year that M. Jules Marcou had discovered and described
a remarkable deposit of fossil plants in the Nebraska territory, which,
from its position, appeared to be unequivocally Cretaceous, although
the forms were considered by Professor Heer to be of decidedly
Miocene character. JI have now before me an interesting notice on
the position of these leaf-beds of the Nebraska by MM. Capellini and
Heer, the former of whom visited and examined them in 1863, while
the latter gives a detailed account of the species. Notwithstanding
his first conviction that the beds containing the vegetable impressions
belonged to a Tertiary formation, M. Capellini was convinced by sub-
sequent examinations that they occurred at the base of the Cretaceous
beds, well marked by the abundance of Jnoceramus problematicus.
The vast extent of country over which these beds occur in an undis-
turbed horizontal position precludes the possibility of any inversion
of the strata.

The following observations of Professor Heer, before describing the
species, will be read with interest. The collection consists of 16
species (all leaves), four of which are badly preserved. They are all
dicotyledonous, and we may in all probability refer 1 to the genus
Ficus, 1 to Saliw, 1 to Diospyrus, 2 to the genus Populus, and 2 to
Magnoha. These are all living genera, and are also found in the
Tertiary formation. Comparing these Nebraska plants with the Cre-
taceous plants of Europe, we find no identical species ; even the
greater part of the genera are different. The Cretaceous flora of
Hainaut in Belgium, and those of Blankenburg and Quedlinburg, are
also quite different. The Cretaceous flora of Moletein in Moravia
offers a greater resemblance ; it contains 2 species of Ficus and 2
of Magnoha. There exists, therefore, a certain relationship between
the Nebraska flora and that of the Upper Chalk of Europe, although
there are no identical species, Hitherto, however, the genera which

Xx¢li PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

characterize the Cretaceous flora of Europe have not been found at
Nebraska.

If we compare the plants of the Nebraska with the Tertiary plants
we find no identical species, but seven genera (Populus, Salix, Ficus,
Platanus, Andromeda, Diospyrus, and Magnolia), which are both
Miocene and still living ; thus the flora of the Nebraska is more
closely connected with the Tertiary than with the Cretaceous flora of
Europe. We must also remember that we are acquainted with only
a small number of the American species, and, on the other hand,
that the Cretaceous flora of Kurope is more allied to the Tertiary flora
than was generally supposed. In the Cretaceous flora of Moletein
in Moravia are found Ficus and Magnolia, which resemble Tertiary
species; one of the Myrtacew, resembling the Eucalyptus rhododen-
droides, Mass., of Monte Bolea ; a Juglans, and a Laurinea, analogous
to those of the Tertiary flora; a Pinus, and two other Conifere
belonging to the genus Sequoia, very abundant in Europe and
America during the Miocene period, = which is now found only
in California.

As the Cretaceous fishes more eee resemble the Tertiary than
the Jurassic fishes, the Upper Cretaceous flora is also quite distinct
from the Jurassic, and is more allied to the Tertiary flora; and it
appears that in America there is a closer connexion between the
Tertiary and the Cretaceous floras than in Europe.

It is very remarkable that the plants of the Nebraska bear so
much resemblance to the living flora of America, whilst the Cretaceous
flora of Europe has rather an Indo-Australian character. Thus it
appears that since the Chalk period the flora of America has not un-
dergone so great a change as the flora of Europe ; and whilst the
Cretaceous flora of Europe is altogether different from the living
European flora, that of Nebraska contains eight genera which are
still living in America; and it is remarkable that the greater part of
them are still found in the same latitude.

I find in one of the last numbers of the ‘ Proceedings of the
American Philosophical Society, held at Philadelphia’*, an interest-
ing account by Mr. Lesley of a recent discovery of Lignite in iron-
ore at Pond Bank, in Franklin County, Pennsylvania, and in which
he describes the importance of the discovery in a theoretical point of
view. Only one similar discovery had before been made, namely, in
Vermont, and, as Mr. Lesley observes, they reopen the discussion of
the age of the present Silurian, Devonian, and Carboniferous surfaces,
and suggest an entire revolution in the generally accepted modes
of regarding the production of Appalachian topography. The Lignite
was struck in a shaft 40 feet below the surface; it contains large
logs of wood, which is partly converted into a brilliant cannel coal,
and the rest of it into common brown coal. Its extent is by no
means considerable ; and Mr. Lesley, dissenting from the views of
Professor Hitchcock, describes it as a mere plug of coal thrust ver-
tically downwards into a mass of clay. It is closely associated with

* Vol. ix. p. 463,

~ ANNIVERSARY ADDRESS OF THE PRESIDENT. xclil

the great belt of iron-ore or hematite which extends along the great
valley for many hundred miles in Pennsylvania and Virginia; but
he is anxious to show that the Lignite and the iron-ore are neither
of the same age nor possessed of any structural attribute common to
both.

Mr. Lesley considers that it is the extreme rarity of these Lignite
apparitions in one of the most wonderfully continuous, extensive, and
valuable ore-belts of the world that gives them all their importance ;
and, notwithstanding the contrary eee of Dr. Hitchcock, he
maintains the importance of carefully separating these sporadic
occurrences of Lignite from the general occurrence of the iron-ore.

In describing the principal features of the great ore-belt of the
Atlantic States along the Great (Lower Silurian) Valley, which
begins in Canada and ends in Alabama, he shows that it belongs
geologically to the Lower Silurian limestone formation. It consists,
however, of two parts—the one stratified as the Silurian limestones
themselves, the other as a surface-wash over the basset edge of the
first. The date of this latter may be Tertiary, or even later. The
stratified portions must be of Lower Silurian age; but the meta-
morphism which they have undergone 7n situ, productive of stratified
clays and ores, may date from any time subsequent to the formation
of a surface-topography approximately identical with that which now
exists. The actual change of the original Lower Silurian calcoferrife-
rous sandstones and slates in situ into limonite-clay beds in ipso situ,
stratified as before, but charged with anadditional percentage of theox-
_ idesfrom a former higher surface now eroded, and with this extracharge
of iron and manganese carried by percolation down to, and crystallized
against, their foot rock, may have required an immense time for its
completion, and was no doubt going on pari passu with the degra-
dation of the surface by slow erosion from higher to lower levels.
He then shows that this long era of iron-cre concentration in the
Lower Silurian slates could not have commenced until after the close
of the coal-era, and probably at a much later period.

The author then describes the exact geological position of the two
great belts of iron deposit, the one at the point of contact between
the Lower Silurian limestone and the overlying slate-formation, for-
merly a deposit of ferruginous mud; the second between the under-
lying slate and the lowest sandy layers of the limestone, lying along
the foot and part way up the side of the south mountain. In one of
these deposits in Pennsylvania the lignite has been found.

He then alludes to the system of underground caverns, which may,
without much exaggeration, be called a single cave, extending for a
thousand miles and including chambers, some of which, like Weir’s
Cave, have acquired a world-wide celebrity. Many of the brooks
descending from the mountain-sides sink into these caverns. The
river drainage on the surface and the cavern system below tell one
story, namely, the extra dissolubility of this particular horizon of Lower
Silurian rocks. The fissures which are now being enlarged into
caves, and the caves which are fast growing into catacombs, their
roofs every now and then falling so as to produce funnel-shaped sink-

XclVv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

holes in the fields, and sometimes in the roads, recciving leaves, fruit,
branches, shells, and other substances with every great spring-freshet
—all these once had their analogues in time past.

The author then submits that, by thus reconstructing the older
surfaces, we obtain.a reasonable explanation of the sporadic masses
of lignite, two of which are now known to exist in, or rather near, the
iron-ore. It is only necessary to suppose a sink-hole so formed and
so stopped up below as first to receive and then to retain an accumu-
lation of forest-trash, and we have the thing ready made to our hand.
The author then proceeds to describe in detail the ore-banks of Mont
Alto, and the relationship of the lignite to the ore. The ore is in fact
nothing but the residue of the Silurian slates and sandy limestone
beds after decomposition and dissolution, after the lime has been
washed out and their carbonated and sulphuretted iron has been hy-
drated and peroxidized, the muddy slates forming the present de-
posits of small ore with white and red clay, while the sandy limestone
formed the present harder siliceous rock ore-belts. He concludes with
some statistical details respecting the enormous masses of hematite
contained in this remarkable formation.

As showing the intensity of geological changes now in operation,M.
Jules Marcou gives an account, in the ‘ Bulletin de la Soc. Géol. de
France,’ of the result of his observations on the Falls of Niagaraafteran
absence of fifteen years. Some of these changes are very remarkable.
Looking at the falls from the Victoria point on the Canada shore, he
says that he could not observe any sensible change in the fall on the left
of the spectator, which is the American fall; but he was much struck
with the changes which had taken place in the great fall to the right,
known as the Canadian or horseshoe fall. The horseshoe form,
_ which was tolerably regular in 1850, has been greatly modified, being .
considerably worn away and deepenedin the centre. The table rock
has almost entirely disappeared; also the tower known by the
name of Terapine is nearer to the edge of the fall, on which side the
mass of water appears to have increased, while it has diminished in.
volume near the table rock ; there also appears to be a slight dimi-
nution in the volume of water passing by the American fall, be-
tween the American side and Goat Island.

He thus tabulates the results of his observations :—

1. The American fall retreats very slowly, and, compared with
the Canadian fall, might be said to be almost stationary.

2. The volume of water in the American fall is constantly decreas-
ing, and will continue to decrease in proportion as the Canadian fall
retreats ; and when the latter shall have reached the islands of the
Three Sisters, viz., in eight or ten centuries, no more water will
pass by the American fall. Goat Island will be jomed to the
mainland.

3. The Canadian fall is rapidly retreating, although it is impossible
to give any rule of its annual retrograde progression, which varies
from year to year. :

4, The mass of water in the Canadian fall increases as it diminishes
in the American fall, besides which it is leaving the Canada shore,

“ANNIVERSARY ADDRESS OF THE PRESIDENT. XCV

and is carried more towards Goat Island and the centre of the horse-
shoe; from which he concludes that. the retrograde movement of the
Canadian fall will be more and more accelerated ; that the valley of
denudation of the river will approach Goat Island, and will then turn
to the east with an abrupt angle as at the whirlpool, and that an-
other whirlpool will be formed at the very spot where the Canadian
fall is now placed.

He concludes his paper with some remarks respecting the strati-
graphical relations of the rocks through which the river flows above
and below the falls.

Amongst the more important works which deserve notice on an occa-
sion like the present, I must not omit the ‘ Geological Description of
New Zealand,’ by Dr. Hochstetter, who, as geologist, accompanied
the expedition of the Austrian frigate ‘ Novara’ round the world.
The work consists of a large quarto volume in two parts, the first of
which is called ‘ The Geology of New Zealand,’ the second ‘ The Pa-
leontology of New Zealand.’ In the very interesting introduction to
this work Dr. Hochstetter shows that the three islands belong to one
and the same system, marked by a characteristic line of elevation
from §.W. to N.E. interrupted by Cook’s Straits between the two
principal islands. This mountain-chain of true alpine character forms
the backbone of the islands, and is said to consist of zones of strati-
fied and unstratified mountain-masses of different ages, which have ~
been raised by plutonic action. It is accompanied, in the northern
island at its western base, and in the southern island at its
eastern base, by zones of volcanic rocks, which have been affected
down to the latest periods by deep-seated igneous action. The lofty
formations of the volcanic zones, and new Tertiary and Quaternary
sedimentary deposits, have given to these islands their present form ;
which is, however, even now undergoing constant changes, both from
earthquakes and from still continuing elevations and depressions.
The geological maps of these islands, even in their still imperfect state,
as compared with the detailed geological maps of western Europe,
show a very great variety of formations ; and although it may not

-yet be possible to establish an exact parallelism between them and
the order of formations in Europe, there is already sufficient evidence
to prove that the stratified rocks of Europe have here their represen-
tatives from the oldest metamorphic formations to the newest sedi-
mentary deposits, and that the eruptive formations extend from the
oldest plutonic rocks to the most recent volcanic lavas.

He considers that New Zealand, with its peculiar living fauna and
flora, differing so completely from the neighbouring regionsofAustralia,
the South-Sea Islands, and South America, is admirably adapted for
testing the correctness of the theory of Professor Agassiz, that no
specific identity can be shown between animals living at a great dis-
tance from each other, even when they existed contemporaneously ;
but that rather genera of the same family, even when belonging to
different geological periods, are more closely allied to each other when
they belong to the same latitudes than those of the same geological
age, but which are derived from different geographical zones.

xevl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

With regard to the marine fauna, it appears from Dr. Zittel’s ex-
amination of the fossils that the molluscous fauna of the younger
Tertiary deposits is closely allied to the living fauna, very much in
the same proportion as that of the Subapennine formation of Italy is
allied to the existing fauna of the Mediterranean. The same genera
occur, both fossil and living, and even the species are not unfre-
quently identical; at the same time they have a great resemblance
to the Tertiary fossils of Chili and Patagonia. described by Sowerby
and D’Orbigny, 7. ¢. to a fossil fauna of the same age and from the
same degree of latitude.

But if we consider the remains derived from older formations, we
find that the Ammonites, Belemnites, Inoceramus, &c. of the nor-
thern island, which belong to the upper beds of the Mesozoic period
(Jura and Chalk formation), so closely resemble European forms of the -
same age, that one is almost tempted to look upon them as European
species ; more particularly the Belemnites, belonging to the group of
the Canaliculati, D’Orb., so completely agree with the Belemn.
canalicalatus, Schloth, that it is almost impossible to find sufficient
differences to justify the adoption of a new name. Moreover, the
oldest fossiliferous beds which are found on the southern island, not
far from Nelson, contain the genera Monotis and Halobia, which can-
not be distinguished from the European forms Monotis salinaria and
Halobia Lommeli, Wissm., from the Trias of the Alps.

Dr. Hochstetter observes that these facts, if confirmed, would go
to prove that the faunas of former periods show an affinity and a
correspondence in the northern and southern hemispheres which do
not exist in the now living faunas—a conclusion hardly in accord-
ance with the above-quoted views of Agassiz, but quite in harmony
with the more generally prevailing opinion, that the older the for-
mations are, the greater is the resemblance in their fossil remains,
even in districts at a great distance from each other.

He then gives a general view of all the different formations, with
their respective subdivisions in New Zealand, from which he con-
cludes that ‘“‘ at the period when the neighbouring Australia, which
was (at least so far as relates to those portions which consist of Pale-
ozoic formations) one of the oldest continents of the earth, rose above
the waters of the ocean, certain portions of New Zealand also ap-
peared as rugged land above the ocean; in a different form, it is
true, from what it now presents, and possibly in connexion with
vast continental masses which have long ago been again submerged.
But while Australia, in its eastern and western portions, has been
little, if at all, disturbed since the conclusion of the Paleozoic period,
so that animals and plants could live and reproduce themselves
in an unbroken sequence down to the present day, New Zealand, on
the contrary, was, even to the most recent period, the theatre of
gigantic terrestrial disturbances and powerful terrestrial conflicts,
which, continually changing the original form of the land, have
gradually given it its present configuration.

After these general views, the author proceeds to give a detailed
account of all the geological features of the north and south islands,

ANNIVERSARY ADDRESS OF THE PRESIDENT. x¢cvli

describing first the physical features of the different regions, and
then their respective geological formations in the following order :—
1. Paleozoic; 2. Mesozoic; 3. Cainozoic, divided into brown coal-
beds and marine deposits; 4. Post-tertiary formations; 5. Volcanic.

Amongst the volcanic phenomena hot springs and fumarole are
most remarkable, and developed to an extent which can only be
compared with the analogous phenomena in Iceland. Both the
chemical and mechaniéal features in these hot springs are identically
the same, notwithstanding the vast distance by which they are
separated. Another remarkable fact is, that the crystalline, or
metamorphic rocks, as well as the igneous rocks, as granite, syenite,
&c.; which form so important a feature in the southern island, are
altogether wanting in the northern island.

The second part of this work contains, as I have said before, an
account of the Paleontology of New Zealand, and consists of the
following monographs :— ) |

I. Remains of Fossil Plants, with 5 plates, by Dr. Franz Unger.

II. Fossil Mollusca and Echinodermata, with 10 plates, by Dr.

Karl Zittel. The Brachiopods, by Edward Suess.

III. The Foraminifera of the Tertiary Greensand of Orakei Bay,

near Auckland, with one plate, by Felix Karrer.

TY. Fossil Bryozoa from the Tertiary Sandstone of Orakei Bay,

near Auckland, with 4 plates, by Dr. Ferdinand Stoliczka.

Y. The Foraminifera of the Tertiary Marl of Whaingaroa Har-

bour (Auckland), with 4 plates, by Dr. Guido Stache.

VI. Report on an almost perfect skull of Palapteryx, with 2

plates, by Dr. Gustav Jaeger.

Dr. Stache concludes his interesting monograph (No. V.) with
some important generalizations, and shows that this foraminiferous
fauna belonged to two groups, evidently derived from two different
sea-depths ; and with regard to their geological age, he shows that
they bear the greatest resemblance to the Neogene fauna of the
Vienna basin, whilst at the same time there are indications of an
older period, approaching the Upper Oligocene beds of the north
of Germany. ,

I must now direct your attention to a work entitled ‘ Frost and
Fire,’ oy Mr. J. F. Campbell, which will be read with satisfaction
by all who are interested in the physical causes which have led to
the structure of the earth’s surface. Although the style of the work
is somewhat quaint, and the arguments occasionally slightly obscure,
we cannot but admire the energy and perseverance with which the
author pursued his researches after the causes, whether heat or cold,
frost or fire, which have been at work as the tools and forces which
have shaped the earth’s crust, either by denudation, deposition, or
upheaval. .

Starting from various physical calculations, balloon observations,
and the temperature on high mountains, he assumes that a low tem-
perature exists in the space through which the earth travels. De-
scending from these outer regions, through “ air,” “water,” and
“rocks,” to mines, he finds that the temperature increases towards the

VOL, XXII. g

XCVlll PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

earth’s centre, while hot springs and lava-currents indicate still
greater heat below the mines thus reached. Thus between attain-
able limits we find cold outside and heat inside the earth’s crust
composed of ponderable materials, all of which, either separately or
combined, can, and do, exist in three conditions—namely, gaseous,
fluid, and solid. Many of these materials are gaseous when heated,
solid when cooled, and fluid at intermediate temperatures. Hach
melts and freezes, or solidifies at-definite degrees of heat, and they
vary in dimension and specific gravity according to temperature.
Heat is force, according to modern views; and rays from the sun,
from luminous substances thrown out from the earth, and from
artificial sources of light, include heat-rays, and are consequently
mechanical forces. Thus force radiates with light and heat from
heated centres, causing expansion, and separating particles from
each other.

Many examples of this action are given by the author in illustra-
tion of these views, drawn partly from natural phenomena, and
partly from experiments ingeniously contrived by himself; a full
description of the cooling of silver is given at p. 346, vol. 11., as one of
the neatest experiments to illustrate the cooling of a molten mass.
The same forms which he has observed growing on cooling slag,’
iron, silver, &c., he finds repeated on a larger scale in cold lavas, in
hot and cold mountains, and in old igneous rocks in Iceland. He
also alludes to the experiments recently made respecting the sun’s
atmosphere and the substances supposed to exist there, and to the
gradual cooling of the different bodies which form our planetary
system ; and assumes that the earth, which is intermediate in size, 1s
also in an intermediate state, partly fluid, partly solid, cooling, but
still hot within. :

Thus he assumes from the facts brought forward that an igneous
foundation is the base on which the sedimentary rocks were de-
posited and now rest; he also assumes that air and water, steam and
ice, moved by the two opposing forces, heat within and cold without,
levitation and gravitation, have worn down the outer crust of the
globe, and have sorted the débris, while movements in the igneous
foundation, and heat radiating and transmitted from it have dis-
turbed and altered the sedimentary deposits; he also considers
that these causes have greatly diminished in intensity since they
first began to act on the crust of the globe. He has illustrated by
numerous drawings and descriptions the marks made by rivers,
waves, currents, glaciers, &c., as well as those made by other de-
nuding agents still at work.

He also assumes that in late geological periods the earth has
cooled so far as to freeze water everywhere at the surface, were it not
for heat radiating to it from the sun. We have reached a partial
glacial period, and the position and extent of ice on the earth now
depend on the amount of heat absorbed from the sun, and on move-
ments in the igneous foundation or centre of the earth.

Some interesting experiments are also shown towards the end of
the second volume to illustrate the effects of the earth’s rotation on

ANNIVERSARY ADDRESS OF THE PRESIDENT. X¢clx

the currents of the ocean, and thus point out the course which
arctic currents would have taken at a period when a larger portion
of the rorthern hemisp ere was submerged. The traces of these
ancient cu reats are to be fourd in the scratchings and strize which
mark the rocks of Scandinavia and Great Britain, and other parts of
Kuiope. There is no ice near the equator; perpetual ice near the
poles, and more in winter than in summer, because of the earth’s
position ; but it is owing to subterranean movements that ice for-
merly extended to lower latitudes in certain portions of the globe.
Thus he shows that in consequence of a recent elevation of the fun-
damental .ocks of Europe, and a probable sinking elsewhere, the
waters which formerly covered certain parts of the surface have
changed their position. The arctic stream, which flowed south and
west, was thus diverted from those districts in Western Europe
which have been raised above the level of the sea to the western side
of the Atlantic; and with it have been carried those vast masses of
ice and snow which formerly scratched and striated with their rocky
contents the surface of Scandinavia and North-western Europe, de-
positing great boulders on their way, and which now condense,
chiefly on Greenland, Labrador, Newfoundland, and North America.

Having thus endeavoured to explain the general theory of the
author, I will merely state that the first volume is chiefly devoted to
an aecount of the denudation of the earth’s surface, the engines by
which this has been effected, viz., frost and ice, and the tools which
have actually done the work, glaciers, icebergs, and Arctic currents,
as represented in Scandinavia, Iceland, Switzerland, and elsewhere.

The second volume continues the history of the same subject of
denudation in the British Islands and America; and the author then
proceeds to consider the question of deposition, the result or counter-
part of denudation, inasmuch as the material removed by denuda-
tion from one place must be deposited somewhere else. Finally,
the question of upheaval is also examined, and its causes and results
duly considered; this, of course, is considered as the effect of the
other great agent in modifying the earth’s surface, viz., fire or heat.
It is illustrated by many ovservations and experiments, drawn from
the furnace and the smelting-works. These results are shown to be
identical with the effects produced by volcanic action, indicating the
existence of great central heat, causing disturbance of the earth’s
surface by earthquakes, and producing upheaval of vast regions by
the expansion of subterranean matter.

Bué without going further into these dynamic questions, or dis-
cu~zing the probable correctness of some of his physical assumptions,
I will merely refer to one point, to which Mr. Campbell’s attention
se’ ns to have been particularly directed, I mean the striation and
grooving of rocks by ice-action. Deeply interested in this question
by the similarity of evidence found in so many countries, and the
apparent parallelism of these strize over vast regions of the earth, he
has collected, partly by his own personal exertions and partly from
the writings of others, a mass of evidence by which he has endea-
voured to throw light on the causes of these Lara: Thus,

g

Cc PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

working his way back by analytical reasoning, calling to his as-
sistance meteorological as well as geological evidence, the laws of
physical science, and the counteracting influence of the two op-
posing forces heat and cold, he comes to the conclusion that these
marks are the result of glacial action ; and by further reasoning on
the various phenomena above alluded to, he concludes that they
have been caused by ice borne by an arctic current flowing from
north-east to south-west. The denudation of the rocks in many
parts of Sweden is enormous, but rivers and weathering will not
account for this. The author observes (vol. i. p. 103) that “on the
watershed not far from Tann Foss at the roadside (at a height
which Robert Chambers estimates at 2000 feet) the clearest marks
of glacial action are still perfectly fresh on rocks, in spite of weather
and rivers. These marks prove that ice travelled over the hills from
north-east to south-west, now 2000 feet above the present sea-level,
at the place where streams now part and run to the Baltic and to the
Atlantic.”

_ As Scandinavia is now generally admitted to be rising from the
sea, there is nothing preposterous in assuming that the greater part,
if not the whole, of Sweden may once have been covered up by the
waves of an arctic sea, in which currents must have existed, flowing,
as now, in different directions, from north and south, according to
those physical laws by which the movements of the ocean-currents
are still regulated.

But the question of land-glaciers flowing down from high regions,
and partly excavating the valleys down which they flow, and leay-
ing their marks also in the shape of scratchings and strie on the
rocky flanks of the valleys, is not overlooked by the author; and on
this subject also much valuable information may be gleaned from
the pages in question. I will only add, that the many illustrations
contained in this volume, and the quaint sources from which the
author has sometimes drawn them, render his work one of great
interest, and which it is impossible to peruse without deep thoughts
and suggestions being forced on the reader’s mind.

Before concluding these observations, I wish to bring to your
notice one or two points which appear to me to merit the serious
attention of geologists in the present day. Prof. Ramsay, in his
Anniversary Address from this chair, alluded to the breaks in succes-
sion of the British Paleozoic and Mesozoic strata, and suggested the
probability that these breaks represented periods of time even longer
than those to which the various existing fossiliferous formations of
Great Britain bear witness. Dr. Bigsby also not long ago brought
under our notice a very interesting paper on missing sedimentary
formations from suspension or removal of deposits, in which he
has pointed out many of the breaks or gaps which occur between
older and younger rocks, caused either by the subsequent removal
of the intervening or missing beds, or because the older beds had
been raised above the sea during the deposition elsewhere of the
intermediate beds. Now it is well known that these breaks or gaps
are only local; and the remark has been already made that, if we

ANNIVERSARY ADDRESS OF THE PRESIDENT. Cl

could only get a sufficient number of sections from all parts of the
world, all these local gaps would be filled up, and we should have
one unbroken sequence of formations, occurring in some part or
other of the earth’s surface, from the lowest Silurian or even Lau-
rentian beds to the most recent Tertiary or Quaternary deposits. . It
would be an interesting task for any geologist to undertake to
supply this want, and to point out the gradual succession of beds
where they can be found, showing how they pass almost insensibly
from one into the other, as the Rheetic beds are now shown to form
an intermediate zone or passage from the Keuper to the Lias. We
should then see by what almost insensible gradations the crust of the
earth has been successively formed, and what were the conditions of
life, or some of them at least, which led to the gradual introduction
of new forms of life in some places, and their partial extinction in
others. And as we have now learnt to recognize the fact that the
extinct Mammalia of the Postglacial period had not all ceased
to exist before the first appearance of man, we should also probably
learn that at no period of the earth’s history were all the forms of
life destroyed before the introduction of new ones ; but that a partial
renewal only took place, and that somewhere or other the witnesses
of one period lived on with the new creations to keep up an un-
broken chain in the history of organic life from its earliest dawn to
the present day.

Another point to which I would invite attention is one of greater
difficulty ; it requires the serious aid of chemistry, mineralogy, and
the laws of physical forces. The study of the older crystalline and
metamorphic rocks has of late years greatly occupied the attention
of many of those geologists who have examined the chemical and
mineralogical conditions of formations. We are told that heat alone
could not have produced the results we see; that water was an
essential element in all these metamorphic operations ; and we find,
in the works of Sterry Hunt, Daubrée, Evan Hopkins, Delesse, Desor,
and others, that even a high degree of temperature was not always
necessary to produce these changes. Many of those results which
have hitherto been considered as the effect of igneous action, are
now believed to be owing to chemical action continued through long
periods of time. It therefore appears that the time is come when
it is desirable to investigate this question; whether the theory of
central incandescent heat is tenable? Whether the plastic condition
of the earth, to which its oblate spheroidal form has been attributed,
be not owing to an aqueous rather than to an igneous origin?
Water is an essential element in every rock, not only mechanically
but chemically ; and without attempting to revive the doctrine of the
Wernerian school, it may be questioned whether we have not some-
times been disposed to overlook the importance of the part it has
played in the construction and solidification of our earth.

Another important subject arising out of this question, or rather
accompanying it as a corollary, would be, whether the solidification
of the earth began at the circumference, after its formation, as is
assumed by the advocates of the central-heat theory, or whether the

cll ‘PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

formetion of the earth may not haye commenced with a central
nucleus consisting of an aqueous paste, gradually increasing in size
as matter was deposited around it from the cireumambient fluids
and gases which filled the solar space before solid matter was aggre-
gated round those spots which now form the planets in our solar
system. It isa bold, perhaps even a rash thought, to go back to a
period before the earth was formed; and yet such a period must have
existed, or the earth would be eternal, which we have no right to
assume. I will also venture to suggest one other question.

Assuming the possibility of an aqueous origin, and eliminating the
theory of central heat, can we not account for all the volcanic and
igneous phenomena which we find on the surface of the earth by
chemical action taking place at a comparatively moderate distance
below the surface? We know that heat and combustion can be thus
produced, and we know that all the elements which are necessary
for its production must have been contained within the earth’s
sphere.

But I will say no more on a qvestion which requires so much
close examination and cautious inves.ization. I recommend it to
your consideration, in the hope that at no distant period some one
will ventue to grapple with it in earnest, and either point out the
probability of what I have suggested, or prove its impossibility.

In-conclusion, allow me to trespass on your time for a few mo-
ments longer, for the purpose of expressing my thanks to every
Fellow of the Society, and particularly to the Members of the Council,
for the kind support and assistance which, during the time I have
occupied the chair, [ have invariably met with at their hands. I am
well aware of my many shortcomings, but, having ever taken a lively
interest in the prosperity of the Society, I trust that this has not
suffered during my Presidency. I look with confidence to the rapid
increase of our Members, in the hope that that is the best proof
that your interests have vot suffered at my hands. I congratulate
you on the choice of my successor, which you have this day made,
feeling confident that, with such a President as you have to-cay
elected, the Society will continue to flourish as it has hitkerto done,
to add fresh laurels to its brow, and that it will continue to hold
that high estimation in the opinion of men of science in every
country which it can confidently boast of having hitherto invariably
enjoyed.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

NovremBer 8, 1865.

Thomas Wiliam Danby, Esq., B.A., Downing College, Cambridge ;
William Poole King, Esq., Avon Side House, Clifton, Bristol; James
L. Lobley, Esq., 50 Lansdowne Road, Kensington Park; John
Richardson, Esq., C.H.; James Clifton Ward, Esq., Clapham Com-
mon; and Samuel Hansard Yockney, Esq., Mem. Inst., C.E., were
elected Fellows.

The following communications were read :—

1. On the Susmercep Forest-Beps of Portock Bay. By R. A. C.
Gopwin-Avsten, Esq., F.R.S., For. Sec. G.S.

ConTENTS.
I. Geology of the District. 4, Surface of Plant-growths.
II. The Forest-beds. 5. Blue Mud-deposit.
1. Introduction. 6. Submerged Forest.
2. The Shingle. 7. Angular detritus.
3. Marine silt. III. Conclusion.

§ I. Guotoey or tHE District.

Portock Bay is the seaward opening of a small valley ; from Hurl-

ston across to Gore Point is a distance of about three miles; its

extent inland is five miles. The valley is bounded on the N.N.E.

by North Hill (1030 ft.), Grabbist (960 ft.) separating it from the
VOL, XXII,—PART I. =

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 8,

-

Minehead valley ; on the 8.8. W. rise Dunkerry Beacon (1678 ft.) and
Porlock Hill; from its position, amidst some of the highest ground
of the West of England, it presents some exquisite scenery, and has
many points of geological interest.

In common with the broad valley between the Quantocks and the

Sketch-map of the neighbourhood of Porlock-.

* Submerged Forest-beds.

Exmoor range, it affords the clearest evidences that the North
Devon and Somerset ranges had acquired their elevations antece-
dently to the accumulation of “‘ Red Conglomerate,” as also of the
Glacial conditions under which the materials of that Conglomerate
were brought together. Surmounting these is the best exhibition
to be met with in this county of the beds of the earliest Jurassic

1865. } GODWIN-AUSTEN—-PORLOCK FOREST-BEDS. 3

period—Sinémurien* (those to which the names Rheetic and Penarth
have been given).

The range which bounds the Porlock valley on the S.W. extends
from the Foreland, by Countesbury to Culbone and Oare, and is the
highest land of Somerset. The mineral character of this great mass
is very distinct from that of the grey slaty rocks, with calcareous
bands and an abundant though obscurely preserved marine fauna,
which extend from Linton southwards in ascending order. From
the valley of the East Lyn to that of Porlock the rocks consist of
hard splintery sandstones, grits, and pebble-beds, with partings of
compact shales—the whole series being of various shades of red. It
is the only portion of the North Devon and Somerset Paleozoic series
which bears any resemblance to the “ Old Red Sandstone” group
of Wales and Gloucestershire. In many respects these rocks recall
characters of parts of the Coal-measures, or of the Lower Wealden
beds.

No animal remains have ever been met with from any part of the
beds of the Countesbury series ; plants have been found, and I have
seen specimens which, though insufficient for description, left no
doubt as to a terrestrial vegetation.

It is difficult to fix the place of the Countesbury rocks in the great
Paleozoic series. The thought that they might belong to the true
“Old Red Sandstone” age made me examine the sections along the
East Lyn valley ; but whereas the true ‘‘ Old Red” everywhere in
the West of England passes up into the Carboniferous group, this
older Red, after one or two alternations, is surmounted by the ma-
rine Devonian series.

The pebble-beds and coarse grits of the Countesbury rocks indi-
cate a shingly coast-line at no great distance. The absence of ani-
mal remains, and the presence of terrestrial plants, suggest that these
may have been the depositions of a lacustrine area, older than the
marine Devonian series of Southern Europe; yet, for all that, they
need not be older than the lower “ Old Red” of Glamorgan, Mon-
mouth, and Hereford.

The great mass of the Countesbury and Dunkerry range has been
produced by a great flexure, of which the steep slope is on the N.N.E.
with an angle of 28°. The nature of the beds, and their highly in-
clined positions, are alike favourable for their deep disintegration.

§ II. Tue Forzst-peps.

1. Introduction.—The whole of the coast-line of Britain is fringed
with submerged forest-ground. Large tracts of it occur in the west:
in Jardigan, St. Brides, and Swansea bays. On the south side of
the Bristol Channel are those of the great Bridgewater levels, which
extend seawards, well described by the late L. Horner, Dr. Buck-
land, and Mr. Conybeare; subsequently by Sir Henry De la Beche
in his Report on Devon and West Somerset.

It has been long known that there was “submerged forest”

* Quart. Journ. Geol. Soe. vol. ii. p. 5.
B2

4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 8,

beneath Porlock Bay: it is indicated in the Ordnance Map of Great
Britain, as also in the Admiralty chart. Sir H. De la Beche gives
the following short account of it :—

«‘ At Porlock a small submarine forest is well exhibited at very
low tides, the stumps of trees, which appear chiefly oaks, standing
in the positions in which they grew. The present action of the sea
has bared these trees, by removing the sand and silt which once
covered them, as can be seen by the continuation of the same bed
of vegetable matter inland, beneath sand and silt, behind the pre-
sent shingle beach, that merely reposes on the inclined plain of the
submarine forest*.”

From a recent examination, the evidences of geological changes at
this place appeared to me to require somewhat fuller detail than is
given in the above; besides which, they better serve to illustrate
the nature and order of oscillations of small amount, which have
taken place at times shortly antecedent to the present, than do the
instances of Bridgewater or Swansea bays.

The Porlock valley, viewed from any of the heights around, pre-
sents at its lowest level a line of coarse shingle, ridged up above
ordinary high water by gales and high tides.

Within this barrier are grassy flats. Further in, these are bounded
by a rise in the ground of from 10 to 15 feet ; above this the surface
of the ground slopes gently towards the hills, forming an under-
terrace to them of variable width, being broadest and thickest oppo-
site the openings of the deep gullies which score the rounded forms
of these hill-sides.

These features are severally connected with the geological history
of the valley.

Within the shingle ridge, broad water-courses have been cut across
the salt-pastures, and good sections of the under-terrace may be
seen along the water-courses, and in the low cliff from Porlock Quay
eastwards. Beyond the shingle, and when tides are low, and the
coast has been swept clean, the Forest-beds are well exhibited. —

The chronological order is as follows (in descending order) :—

Shingle bank.

Marine silt.

Surface of Plant-growth.
Fresh-water mud-deposit.
Forest-growth.

Angular detritus.

2. The Shingle.—The shingle-beach requires passing notice in re-
spect of its position. It is composed wholly of the siliceous rocks of
the coast from Porlock westward, and forms a ridge round the bay.
On the land-side it ends abruptly, as if encroaching on the meadows ;
seawards it thins away, so that at extreme low water but little
shingle remains, and in the offing the sea-bed is composed of sand
and fragmentary shells. ,

The shingle, where now thickest, has been heaped up upon the
surface of the meadows, no marine shingle of earlier date is any-

* Report on the Geology of Cornwall, Devon, and West Somerset, p. 419.

1865. ] _GODWIN-AUSTEN——PORLOCK FOREST-BEDS. 5

where to be seen on the inner or land-side, and the series of deposits
which it overlies show that, with reference to past conditions, the
most recent change has been one of slight depression.

3. Marine silt—On the land-side of the shingle ridge is an ex-
panse of salt-meadows, which at present are but occasionally, par-
tially, and for short intervals covered with water ; their level is at
the very upper limit of the Bristol Channel waters. From the ma-
terials thrown out from the dykes cut across this flat, as also in the
sections thus exhibited, the nature of the subsoil is well seen, con-
sisting of mud-deposits. Of these the uppermost is of a yellowish-
brown colour, and contains the shells of Scrolncularia piperata, with
the valves united, and of all ages. The presence of these shells
shows that the lower part of the Porlock valley was at one time in
the condition of a mud-flat, wholly covered by the sea at every tide,
perhaps even permanently covered—that they were then at or near
the low-water level, or that the area was then depressed to the
extent of the difference between high and low water; the range
of Scrobicularia piperata being from low water to four fathoms
beneath.

Beneath the Scrobicularian mud of the meadows is a band of
vegetable matter, and under that a dark tenacious clay ; these are
better seen on the coast.

4. Surface of Plant-growths.—At low water, and when the coast
has been swept clean of shingle, there is presented an expanse of
mud-deposits, with the stumps of trees studded about. The mud-
deposits occur in patches, owing to the action of the breakers, which
cut out portions; around these patches are good sections.

The uppermost mud-deposit, that with the Scrobiculariz, is not very
resisting, so that it occurs only occasionally over the area left by
the tide ; enough, however, remains to show that it was at one time
spread out continuously, with a like composition and under the same
conditions as are presented by the beds beneath the meadows; as
such it passes down beneath the present lowest water-level. Under
the yellow mud-deposit is a dark band, and when the mud has
been removed, the surface presents a layer of matted vegetable
matter, seemingly composed of roots. This seam is in places several
-inches thick; on the underside roots descend into the subjacent clay,
showing that it has been an old surface of plant-growths.

The stools of trees project slightly above the level of this old land
surface ; and upon it lie the trunks of trees. In every instance that
I examined, the surface of plant-growths was interposed between
the prostrate trunks and the underlying blue clay. There were
stems measuring from 10 to 20 feet and more in length. They
were mostly, if not altogether, the remains of trees which had died,
and become bare of bark, some much decayed before they fell; they
projected above the surface, and had not sunk into it, or the surface
was firm, and not in the condition of a soft morass, when the trees
fell upon it.

The roots and long leaves seemed to belong to an Iris, such as the
common “ Yellow Flag.”

6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 8,

5. Blue Mud-deposit.—This is a very tenacious mass, resisting
the action of the sea. It is of variable thickness, increasing as it
passes down seawards. After most diligent search I was unable to
find any evidence as to the nature of this deposit, whether fresh-
water or marine ; in this respect it resembles the blue-clay deposit of
the Bridgewater levels; from the abundance of diffused vegetable
matter it has the appearance of being of freshwater origin.

It might seem at first sight, as indeed it did to Sir H. De la Beche,
that the trees of the submerged forest had grown in this blue mud,
from the manner in which they stand out of it; but the mud-
deposit swrrounds the stools of the trees, which never send roots into
it; and wherever the mud has been removed the trees are seen to
be rooted in the beds beneath. The accumulation of the mud has
been subsequent to the forest-growth. The uniform level at which
the trees have been cut off may, perhaps, indicate the level of the
water which deposited the blue mud, and killed the trees at the
same time.

6. Submerged Forest.—The interval left bare by the tide may,
under favourable conditions, be seen studded thickly by the stools of
large trees—some bare, some covered by a thick growth of sea-
weed, some just projecting above the mud-beds. Some are of large
size; one measured 2 feet in diameter. The largest trees were
the oaks, which may be distinguished by the black colour of the
wood ; others, when split open, are red, probably alders ; from their
dimensions both must have grown under favourable conditions *.

The prostrate trunks lay generally N.W.,8.E., or away from the
opening of the valley ; they had been broken off without tearing up
their roots.

7. Angular detritus——The flooring upon which the blue mud-de-
posit lies, for as far out as it can be traced, is of coarse angular
rocks, instead of some form or other of water-worn materials, as
might have been expected ; these consisted only of fragments of the
splintery quartzose rocks of Dunkerry, of all sizes, with their
edges and points as sharp, their surfaces as clean as if just broken ;
all thrown together in the greatest confusion. Part of this rugged
appearance may have been produced by the tides having washed
awav some of the finer materials. All the trees are rooted in this
detritus ; it was the surface on which they grew, and had established
themselves antecedently to the changes here noticed. The nature
of this accumulation, if I am right in my explanation, renders the
Porlock Bay forest-beds of more geological interest than the more
extensive tracts of Bridgewater or Swansea.

A thick coating of angular débris covers the surface of all the
hill-ranges of North Devon and Somerset ; it is always strictly local,
and is simply the product of the breaking up of the surface to a
great depth. In places the mass of débris is im sitw,—merely
detached; but along some of the new roads which have been cut
about the sides of these ranges, sections are exposed, showing that

* Large oak and alder characterize the Porlock valley, at present higher up
as along the course of the Horner stream.

1865. ] GODWIN-AUSTEN—PORLOCK FOREST-BEDS, 7

ereat masses or “ trainées” of the débris have come down from
above, cutting deep channels through the detritus at lower levels.

These accumulations of angular detritus along the lower slopes are
of great thickness ; the materials have also been carried forward to
considerable distances, more particularly in advance of deep glens.
The high ground from Countesbury to Dunkerry (1678) and Porlock
Hill has everywhere good illustrations of the character of these
masses of detritus.

A section of such beds is to be seen in a low cliff extending east-
wards from Porlock Quarry, and serves to connect the detrital mate-
rials of the interior of the country with the beds beneath the bay.
It is a section of part of the under-terrace already noticed.

This section, which has a depth of from 10 to 12 feet above the level
of the shingle, shows an accumulation of earthy materials, angular
fragments of all sizes, all derived from the rocks of Porlock Hill.
There is to be noticed a sort of horizontal arrangement resulting
from interbedded lines of finer materials, and showing successive
accumulation. On either side of the place at which a stream comes
down to the coast, cutting through the thickness of angular mate-
rials, there are to be seen, mixed with it, some water-worn, partially
rounded blocks; these indicate the course of a torrential stream from
the high grounds above (as at present), but occasionally of greater
volume.

This accumulation of angular materials is referable to like bygone
conditions as have been already indicated for the whole of the rest
of the West of England (Quart. Journ. Geol. Soe. vol. vii.pp. 121-131).
It is a condition of surface presented everywhere by that portion
of this country, and of Europe, which was not submerged during
the great subaqueous depression of the Northern hemisphere. In
geological history it belongs to the subaérial phenomena of the
“Glacial Period,’ and represents the whole of the variable conditions
of that long interval of time.

III. Concrvston.

Reversing the order of superposition, the sequence of change at
this place is as follows :—
Ist. The formation of angular detritus, and its accumulation at
lower levels.—Highest relative level.
2nd. Forest-growths established on detrital beds.—Trees of
great age.

3rd. Accumulation of freshwater mud, resulting probably from
a depression of the level of the land.—Trees killed.
Ath. Surface of water-plant growths on mud-deposit, or nearly
dry surface, on which the trees fell.
| 5th. Deposit of sea-mud, with Scrobicularia.—Area depressed
below the sea-level.
6th. Conversion into meadow, at the level of the highest springs
at present.
| 7th. Shingle.

8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 8

It may be inferred from Sir H. De la Beche’s description that he
had not had opportunities of distinguishing the two surfaces of plant-
growths, nor the remarkable floor of angular materials on which the
forest-bed is rooted. It is not stated whether the “silt and sand ”’
of the “inclined plane” was freshwater or marine.

The succession of changes here indicated corresponds with that of
numerous other localities at which I have had opportunities of ex-
amining the evidence in the West of England. The Porlock example,
in addition, seems to fix a relative date for a part, namely, as being
subsequent to the great subaérial weathering of the surface during
the Glacial Period. ‘The elevation of the land was greater at that
time than at present, but by how much we have no means of
determining.

The difference of level within which the land has oscillated since
then need not be estimated at more than 40 feet, the range between
high and low water on the Bristol Channel coast being taken at 33
feet. It is certain that such forest-growths as pass on all sides
beneath the line of low water could not have lived at the high-water
level, but a rise of 50 feet would convert the upper part of the Bris-
tol Channel into land-surface. The greatest depth at which sub-
merged land-surface has been ascertained is about 120 feet; a rise
of such amount would place the whole of the Bristol Channel in the
condition of dry land, and such probably it was at the time of the
forest-growths. .

The line of the Bristol Channel is that from which the amount of
depression of the British area in the West increased progressively
northwards, corresponding to the line of the Thames valley in the
East. There is clear evidence that the line of the English Channel
was occupied by sea during the ‘‘ Cold Period” (Quart. Journ. Geol.
Soe. vol.vii. p. 185); and at the Newcastle Meeting of the British Asso-
ciation I indicated to what extent this unsubmerged area of the South
of England was affected by that depression. Like evidence may
now be derived from the coasts of North Devon and Somerset.

The lowest and oldest beds beneath the Bridgewater levels are of
sands and subangular gravel, made up of all the materials of all the
hill-ranges which send their streams towards that depression, from
the grauwacke of Exmoor and the Quantocks up to the Chalk
inclusive.

From the great extent of the old alluvia of this area of drainage, .
the volume of the rivers must at some time have been very great, and
as no part of it was comprised by the line of circumpolar submer-
gence, these alluvia are referable to the subaérial conditions of the
whole of the Glacial Period. The great gravel-beds of the Bristol
Channel, noticed by Dr. Buckland as proofs of his Diluvial theory, -
are the accumulated glacial alluvia of all the rivers of the West, from
the Severn to the Tone: they are the equivalents in age of the great
accumulations of angular débris.

Over the whole of the West of England the remains of the great
Pachyderm fauna occur abundantly in, more generally beneath, the
old alluvia, as also beneath angular débris, at various elevations,

1865. ] WATSON—PARALLEL ROADS OF GLEN ROY. 9

about the Mendip, Quantock, and Exmoor ranges; but there is no
evidence whatever that the great characteristic part of that fauna was
in occupation of the area at more than one period. It became extinct,
even over the area of the South of England, which was not sub-
merged ; indeed the extensive subaérial glaciation which that area -
has undergone from Cornwall to Kent and. Sussex, is inconsistent
_ with the existence of such a fauna.

Lastly, with reference to the age assigned to these later changes,
subsequent to that of extreme cold, a relative date is arrived at for
many of the so-called “ Raised Beaches”’ occurring on our western
coasts. The example nearest to Porlock in the West is that between
Braunton and Baggy Point, long since so well described by Sir R.
Murchison and Professor Sedgwick. At this place there is the evi-
dence of the more recent changes at low levels, the older sea-
bed, at an elevation of 60 feet for its higher portions, being covered
up by an enormous accumulation of angular debris-bed *.

I have already called attention to the great thicknesses and other
characters of the angular débris overlying old sea-bed (Quart. Journ.
Geol. Soc. vol. vii. p. 118), and would also refer to the observations
of Sir H. De la Beche (Report on Cornwall, &c., chap. 13).

In a modified sense these sea-beds or raised beaches are pre-
glacial, or older than the period of deep surface disintegration. But
just as the amount of northern depression increased from South
Northwards, so the progress of that depression was in the contrary
direction, or from North to South ; the line of the Bristol Channel
was nearly the limit of this submergence, and was the last reached.

The interval of time which separates these more recent changes
of relative level from that of the great depression of the Northern
- Hemisphere, is possibly very great, not so their distance from the
present. The distinctive features of the newer deposits are, that they
belong to the time of our existing assemblage of animals and plants,
that they indicate changes of small vertical amount, and are remark-
ably uniform.

2. On the Marine Ortcin of the Parattet Roaps of Gren Roy.
By the Rev. R. Boog Watson, F.R.S.E., F.G.S.

(Abstract.)

THe Parallel Roads of Glen Roy have been described by several
observers, who have also offered explanations of the manner of their
formation. In the author’s opinion, Mr. Robert Chambers has
solved this problem in his ‘ Ancient Sea Margins,’ and in this
paper he supported the view there advocated, and offered some
objections to the theory of an ice-dam, originally put forward by
Prof. Agassiz, and recently illustrated by Mr. Jamiesony.

After noticing the strong points of the ice-dam theory, Mr.
Watson remarks that, though Prof. Agassiz and Mr. Jamieson agree

* Bed a of Section. Geol. Trans. 2nd ser. vol. v. p. 279.
+ Quart. Journ. Geol. Soc. vol. xix. p. 235.

10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 8,

in supporting it, yet they differ so much respecting details that they
mutually weaken their cause*. He then considers the specific
objections to the theory, especially the existence of terraces similar
to the Parallel Roads, though less perfect, at all levelsroundour coasts,
as well as inland, along every fjord in Norway, and across the whole
of Sweden; these, he says, cannot be accounted for by the ice-dam
theory, which therefore treats them as something distinct, whereas
they are specifically the same, differing from the Glen Roy Roads
only in being less perfectly preserved. Mr. Watson also remarks
that, even in Lochaber, there are banks of water-sorted gravel at
various heights and unconnected with any “ col’’—a fact which
cannot be accounted for by the ice-dam theory; and he mentions
particularly two short lines between the two highest roads in Glen
Roy, and one in Glen Gluoy at 960 feet, which do not correspond
with any “col,” also several instances in and near Glen Collarig.
He then describes an extraordinary series of terraces on Ben Clinaig,
and draws attention to certain gigantic flat-topped heaps of water-
sorted gravel, whose levels do not correspond with those of any of
the terraces. Mr. Watson therefore asks, What can the ice-dam
theory do with all these? He also states that if the cold was
severe enough to supply the ice needed for such a dam, it was too
cold in Lochaber for lakes, and vice verséd. Glaciers, he remarks,
are mere tongues of ice projecting beyond the snow-line, and the
area which these tongues occupy is minute compared with that
occupied by the body—the snow-field which contains them ; but
the ice-dam theory reverses this relation, and makes the snow-hody
minute and the tongues gigantic. Mr. Watson also considers that
it was impossible for the ice to be present at the places indicated,
as no glacier from Ben Nevis could reach Glen Roy, and no inde- .
pendent glacier could be formed in Glen Spean. Another objection
is, that no place can be found for the ice-dam theory between the
glacial epoch and the present day—a consideration which the author
discusses in detail, and he concludes his objections by urging that,
as the sea has been all over the Lochaber district to a height of 2000
feet, there is no reason for seeking any other agency for the forma-
tion of the terraces, nor for introducing such a complex machinery
as the ice-dam, where none is needed.

In supporting the “‘ Marine” theory, on the grounds that the sea
has been on the spot, and is capable of performing the work re-
quired, Mr. Watson gives the following sketch of the manner in
which he conceives the “ Parallel Roads” to have been formed :—
«We have the land standing probably, in the first instance, rather
higher than now, but gradually sinking, though perhaps with
pauses. The climate resembled that of North Greenland. The
land was swathed in thick ice, which was ever settling downwards
to the sea, under that law of regelation which gives to ice its true
viscid or plastic character. The whole surface of the rock was being
moutonnéed and striated. The boulder-clay resulting from the
destruction of the earlier soils and looser weathered rock-surfaces was

* See Reader 1864, p. 301 (September 8).

1865. ] WATSON——PARALLEL ROADS OF GLEN ROY. 11

being shot out in heaps beneath the half-floating ice-foot. The
finer clays and older shell-beds are the produce of the somewhat
later and more land-sunken time, when the comparatively cleared
surface of the rock and the shrunken glaciers no longer supplied the
same mass of débris as before. The gales of spring from the 8.W.
came to break up the ice of winter where it lay on the level shal-
lows, such as the long flat of Glen Spean, east of Loch Treig valley,
and piled up the blocks of rock which the ice contained into those
strange and monstrous sea-beaches (see Jamieson’s map) which have
been erroneously described as moraines. And, finally, dependent
on the sheltered nature of the locality, on its exposure to the pre-
valent winds, on the character of the hill face, on the supply of
débris from above, on the extent to which particular spots at the
sea-level were already clothed with detritus under the influence of
the varying currents pouring backwards and forwards over the cols
at the glen heads—perhaps, too, to some extent, acted on by the
ice-cake—subject to all these influences the terrace-lines were
formed along the slopes. Sometimes they were swept away again
almost before formed, or were spared only for later destruction ;
but, in the case of the sheltered fjord of Glen Roy, each terrace in
turn was carried down with the subsiding land, and protected from
injury below the sea in the quiet of the inland fjord, while the next
terrace above it was being formed in its turn.”

That there are some difficulties in the way of the “ Marine
theory ” Mr. Watson does not deny, the greatest, perhaps, being, in
his opinion, the marvellous perfection of the Glen Roy terraces
when compared with anything similar there or elsewhere. He also
discusses two other objections, being all that he thinks need con-
sideration. The first of these is, that the horizontality of the
“roads” is opposed to the idea of their having undergone sub-
sidence and re-elevation ; but Mr. Watson observes that there is no
reason to suppose that any disturbance of relative levels should be
exhibited when areas of thousands or hundreds of thousands of
square miles are undergoing secular oscillations, and he cites in
illustration the beach-lines along the Norwegian fjords. The other
objection has been urged by Prof. Agassiz as his greatest difficulty
in accepting the “ Marine theory,” namely, that the terraces pre-
sent “no traces of organic life”’*. Mr. Watson answers this by
quoting several examples of Quaternary marine deposits which are
also entirely barren of fossils; and he states that it would be sur-
prising if fossils had been found in the Parallel Roads, as he has
noticed that there is, from some cause or another, an extraordinary
gap, utterly devoid of life, so far as we know, between the most
recent of the old glacial beds and the very oldest of the recent de-
posits. The general character of the Scandinavian Quaternary beds
he has found to correspond with that of the Scotch deposits, “and
they also agree in this, that while true glacial shell-beds are to be
found from the sea-level, and below it, up to 500 feet, or a little
more, above it, there they cease altogether. The higher stratified

* Reader, Sept. 3, 1864, p. 301.

12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy, 22,

deposits are utterly devoid of a single organism, and it is not until
we descend again to the height of 200 feet above the sea (in Scot-
land lower still) that we again begin to find fossils, in beds over-
lying the former; but in the shells of these later beds the glacial
character has disappeared altogether.” He holds, therefore, that
the absence of organic remains from the terraces of Glen Roy
simply accords with the character of similarly placed beds in every
other locality, both in Scotland and in Scandinavia.

NovemBer 22, 1865.

Robert Lightbody, Esq., Ludlow, Salop, was elected a Fellow.

The following communications were read :—

1. On some Spaces, formerly occupied by SuLenrtE, in the Lownr
EKocrnr Criays of the Lonpon Basin; with remarks on the OniGIn
and DISAPPEARANCE of the Minerat. By P. Marrm Doncan,
M.B. Lond., Sec. G.S.

me Cc b

ConrTENTS.
1. Position of the spaces and impres- | 5. Considerations respecting the de-
sions in the Woolwich beds. posits.
. Description of the spaces and im- | 6. Origin of Selenite.
pressions. 7. How it is removed from sedimen-
. The mineral condition of the organic tary deposits.
remains in the beds. 8. Conclusion.
. Discovery of the spaces in the Lon-
don Clay.

1. Position of the spaces and impressions in the Woolwrch beds.
—Several sections of the Woolwich beds were made during the
formation of the railroad from Lewisham to Dartford, and the
Ostrea, Cyrena, and plant-beds were well shown. At one spot,
between Mottingham and the Eltham road, the beds had a slight
dip to the south-west, and cropped out on the side of a rounded hill
which bounds a rivulet to the north. The lowest part of the sec-
tion there exposed presented a thick layer of Ostrew, and to this
succeeded several feet of light-brown clay, sandy in places, in which
Oyrene and Melanie were very abundant. A plant-bed followed
being formed by remains of twigs, leaves, vegetable fibres, and long
water-plants. The usual sequence was not then noticed, on the con-
trary, several small plant-beds were observed between the succeeding
clays. Amidst the clay were some impressions which at first sight re-
sembled the markings of verticillate leaves, but which were evidently
parts of spaces once filled by stellate crystals of selenite.

Several lumps of clay were removed for examination, and pre-
sented, when cut into, numerous moulds of entire stellate groups,
but all trace of the mineral which had produced them was gone.

2. Description of the spaces and impressions.—The spaces were from

1865. | DUNCAN—IMPRESSIONS OF SELENITE. 13

1 inch to $inch in diameter, were empty and moist, and were usually,
but not invariably near a plant-bed. The impressions in the clay
were very distinct, sharp, and permanent, and the flatness of the erys-
talline planes was perfectly represented, as was also the sharpness of
the angles. The colour of the clay within and without the spaces was
at first the same, but exposure to the air determined the deposit of
sesquioxide of iron on the plane surfaces. Close to the exterior of
the spaces were numerous spots resembling Entomostracous remains,
but which were of a lighter colour than the clay, and which yielded
to analysis alumina, silica, and sulphide of iron*. When permitted
to dry, some of the hand-specimens showed much alteration near the
selenite impressions, from the replacement of the protoxide by the
peroxide of iron, but none elsewhere. No crystals or lamin of
selenite were found near the spaces. In one space there was a bril-
liant piece of carbon.

The clays were soft and not laminate; they contained variable
quantities of sand, and graduated into a decided loam here and there.
The section proved that the natural drainage through the deposit
was in perfect operation.

3. The mineral condition of the orgame remains im the beds.—The
large Ostree were imperfectly silicified and very hard. The Melanie
were generally very perfect, and were of all sizes: they were either
empty, very fragile, and the carbonate of lime in the shell was tender
in the extreme, or the shell was tough and its interior filled with
erystalline carbonate of lime; or, in a few instances, an imperfect
silicification had produced a cast.

The Cyrene were of various sizes, and were either very fragile and
empty, or their interior was filled with dense carbonate of lime, the
shell being here and there deficient.

The plant-remains were carbonized, and much of the surrounding
clay was stained black, but in some places fibres existed of their
usual colour. |

4. Discovery of the spaces in the London Olay.—Shortly after
these impressions were noticed in the Woolwich beds, several large
moulds of selenite were discovered in the London Clay of the
Tendring Hundred of Essext. They were very numerous, and
were larger than those from the Woolwich beds. The clay in which
they were found was the usual dark blue-grey London Clay, and was
unfossiliferous. The impressions were perfect, very complicated from
the verticillate arrangement of the crystals, and the clay within the
spaces was either perfectly like that without, or after a time became
tinted with the sesquioxide of iron. Very small pieces of selenite
were abundant close to the impressions.

5. Considerations respecting the deposits—Selenite is very common

* The loam when washed with distilled water yielded less than 1 per cent. of
soluble matters. They consisted of chloride of sodium, sulphate of magnesia, a
trace of organic matter, and less than 1 per cent of sulphate of lime.

The finer particles of the loam took very long to settle, and the sediment con-

sisted of silica, silicate of alumina, protoxide of iron, and salts of lime, soda, and
magnesia.

t+ Mr. James Cooke, C.E., F.G.8., obtained the specimens.

14 PROCEEDINGS OF THE GEOLOGICAL socieTy. [ Noy. 22,

in the London Clay, but comparatively rare in the Woolwich beds:
moulds of it have not been hitherto recorded in the first deposit, but
Messrs. Prestwich and De la Condamine noticed them many years
ago in the latter at Counter Hill*.

However common these spaces may be, the facts still remain for
consideration, that a rather insoluble mineral has been deposited in
and removed from sedimentary marine and fluviatile deposits, and
that the mineral has not hitherto been formed artificially. The erys-
talline nature, optical properties, and chemical composition of selenite
are well known; but it is a species which has either been much neg-
lected or has been treated as crystalline gypsum, being considered
to be influenced identically with it by reagents.

The part of the Woolwich bed and that of the London Clay under
consideration, were deposited under different circumstances. Mr.
Prestwich’s great essay has so exhausted the subject, that it simply
remains to state that the one was accumulated during the physical
changes incident to an estuary, and that the other is more or less a
deep-sea deposit.

It is evident that neither the selenite nor the shells forming the
bulk of the deposit near Mottingham were rolled, for the impressions
are sharp, and the fragile shells are usually entire. The shells
belonged to individuals of all ages, they were all jumbled together,
and it is evident that the mollusca did not live quite on the same
area in which their shells are preserved. If it could be allowed that
these masses were washed together to die under some unusual cir-
cumstances, one of which must have been a sudden depression of the
surface, an immense amount of decomposition must have ensued, and
the decaying mass of mollusca, extending over a large area, would
have produced well-marked changes in the lithology of the district.
All the chemico-geologic facts, however, disprove such an amount of
decomposition, and indicate a feeble amount of organic decay. The
water-supply probably consisted of river-water, brackish water, and
occasionally of pure sea-water. The river probably worked its way
through the chalk, and its water was as well supplied with sulphate
of lime as similar streams now are. More of this salt it could not
have had, for the molluscous and plant-life was evidently abundant
and vigorous. The quantity of clay and sand which now forms the
matrix for the shells is but a small vestige of what was deposited
contemporaneously with repeated quantities of shells, and it is most
probable that during the slow depression of the surface of the land
and estuarine bottom, the layers of shells were deposited with great
quantities of silt and clay, which were more or less washed away
from time to time. That is to say, the mollusca were gently washed
into channels and formed a thin layer; they were covered up with
silt and clay, and their decomposition was probably in progress when
another layer was formed above; the greater part of the inorganic
deposit was then washed away, and the layers gradually merged one
into the other; or the succession of layers may have been numerous
before the bulk of the sand and clay wasremoved. ‘This explanation

* Prestwich, Quart. Journ. Geol. Soe, vol. x. p. 123.

1865. | - DUNCAN—IMPRESSIONS OF SELENITE. 15

meets the difficulty of accounting for the slight evidences of decom-
position in the beds which are so crowded with shells.

It must be remembered, in considering the subsequent geologic
chemistry of the beds, that as the depression of the estuarine deposit
proceeded, it was covered with the marine London Clay, and that
salt water percolated through its beds until all was elevated, and
subaérial denudation commenced.

The London clay in the neighbourhood of the impressions is un-
fossiliferous, and contains no carbonate of lime, but doubtless the
organisms common to all sea-bottoms were once present, and deter-
mined in a decided manner the mineral condition of the deposit.
The small particles of selenite near the impressions were probably
carbonate of lime at one period. River- and rain-waters had nothing
to do with these clays at first, for they were washed and percolated
by sea-water, until the elevation of the lower Eocene beds subjected
them to the action of fluviatile and meteoric waters.

The slow rate of drainage through the London Clay is tolerably
evident. It will be noticed that in one instance the evidences of the
deposition and removal of selenite were found in beds which were
shallow- and fresh- or brackish-water deposits, and that a prolonged
exposure to percolation by sea-water was followed by a rapid perfect
drainage by fresh water; whilst in the other instance the proofs were
discovered in marine deposits which were not formed near the sur-
face, and which have been finally slowly drained by fresh water.
Moreover the selenite is common in the marine but rare in the es-
tuarine deposit*, and in both it is scattered and is not in horizontal
layers.

%. Origin of Selenite—There are many instances of the formation
of crystalline gypsum during the recent period, consequent on the
evaporation of waters holding sulphate of lime and other salts, such
as sulphate of soda and chloride of sodium, in solution. Darwin
found large crystals in the banks of a South American salina which
deposited large amounts of sulphate of soda; Bischof and others
notice the formation of laminar crystals on the faggots placed for
retarding the percolation of certain saline waters, and there are some
fine specimens of recent crystalline gypsum impregnated with sand
in the museum of the Society. The deposition of small crystals and
of the amorphous mineral occurs very constantly t.

Now all these deposits occur under somewhat identical conditions,
and often have a relation to the comparative solubilities of the chloride
of sodium and sulphate of soda which are more or less present in the
waters. The excess of sulphate of lime is rarely observed, and it is
pernicious to molluscous life; and as itis not advisable to travel out
of the usual course of things in attempting to account for difficult
natural problems, it may be conceded that no more than an average
amount of the salt is, in the first instance, present in the great ma-

* Mr. Prestwich notices the absence of selenite in the mottled clays of the
Woolwich beds (op. c7z.).

t Chem. and Phys. Geol. Cavendish Society, vol. i. p. 426.

t Ibid. vol. i. p. 154.

16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 22,

jority of instances where it is ultimately deposited by evaporation.
It is very evident that the selenite of the London Clay could not
have been the result of surface-evaporation, for it is found through-
out the thickness of the deposit, which, moreover, is of deep-sea
origin.

In the Woolwich beds the spaces were found, not in layers, but
scattered and at various depths. It is possible that the facilities
for evaporation were occasionally considerable in this deposit, but
there are many reasons to be adduced against this idea.

There are no evidences of either the Woolwich or London Clay beds
having been percolated by an intensely gypseous water. ‘There is a
difficulty in this part of the inquiry in consequence of the difference
between selenite and the other forms of crystalline gypsum.

All the specimens which have resulted from evaporation which I
have seen, cannot be called selenite, they are more fibrous, less
laminar, and not so regularly crystalline. The distinction between
the two forms is acknowledged by some, but ignored by other mine-
ralogists, and Bischof must. be classed amonpet those who consider
all the forms, except Anhydrite, to be identical in the chemico-geo-
logic sense. But although burnt selenite acts chemically hike burnt
gypsum, still in its crystalline form it is infinitely more durable, less
soluble, and less influenced by heat, cold, and moisture. The struc-
ture of selenite infers long periods of time for the perfection of its
large laminate crystals; andif this be the case, it is, especially when
the extra amount of water of composition is considered, a strong
- argument against its origin by simple and immediate deposit.

As there is some doubt whether selenite is ever the result of simple
deposition, the examples now and then presented of selenite crystals
developing in masses of amorphous gypsum, become very important.
In fact the only definite knowledge of the origin of the mineral is
. derived from them, and all other explanations are hypothetical.

Gypsum may have been deposited in the clays from either the per-
colating river- or sea-water; but still this is less probable than its
secondary and chemical* origin by the changes induced in carbonate
of lime by decomposing organic matter. Although carbonate of
lime does not now usually exist per se in the clays, still masses of
it are found here and there, although they have been exposed to
_ great water-washing. ~During the earlier years of the London and

Woolwich beds, ieee amounts of carbonate of lime must have been
formed from the detritus of shells, and in many places they must have
been exposed to the influence of sulphuretted hydrogen, and its asso-
ciated gases—the result of the decomposition of organisms.

If it be admitted that water containing sulphate of lime will pro-
duce an evolution of sulphuretted hydrogen, carbonic oxide, and
carbonic acid gases from dead organic matter, it simply remains to
account for a sufficiency of oxygen to develope small quantities of sul-
phuric acid, before gypsum can be produced from the carbonate of
lime. The constant presence of organisms between the layers of —

* See “ Remarks on the Production of Crystals,” baal John Morris, Mag. Nat.
Hist., November 1837.

1865. ] DUNCAN—-IMPRESSIONS OF SELENITE. i

selenite and amidst gypsum is remarkable, as is also the frequent
neighbourhood of plant-beds or lignites.

It is by no means improbable that the deoxidation of the vegetable
remains before their complete transformation into lignite, may have
been produced by the gases resulting from decomposing contiguous
organic substances in contact with water containing usual amounts
of sulphate of lime in solution. The sulphuretted hydrogen, deriving
oxygen from the vegetable matters undergoing their transformation
into more or less pure hydrocarbons, yielded the sulphuric acid re-
quisite for the formation of the gypsum.

How constantly peat, coal, and several forms of gypsum are asso-
ciated is well known, and the theory should hold good in all
instances.

It would appear then most consistent to assert that the selenite of
the London and Woolwich clays was formed in amorphous gypsum,
the result of the decomposition of carbonate of lime by sulphuric acid
-In minute quantities, probably in percolating water. .

The solution of the gypsum around the crystals of selenite and
the closing in of the clay are inferred to have then taken place.

7. How selenite may have been removed from the deposits.—The se-
lenite must have been removed from the spaces in one of the fol-
lowing manners :— .

1. By being washed out mechanically.
2. By being simply dissolved by percolating waters.
3. By being decomposed.

1. The spaces were all closed, and the clay was not laminated until
it became dry. The impressions of the planes and angles were per-
fect. These facts militate against the removal mechanically.

_ 2. The improbability of the solution of the selenite may be gathered
from the following considerations.

In the same London Clay, in more exposed situations, where con-
stant moisture and sea-spray act in all seasons, selenite is still found
in great abundance. If selenite be not dissolved on the Walton cliffs,
why should it be dissolved inland, where the only moisture is that
of very slowly percolating meteoric waters? Small particles of
selenite remain undissolved close to the spaces, and there is an abun-
dance of soluble matter around them. The hardness and perfection
of the planes and angles of the impressions could not have been ex-
pected after so prolonged a percolation as that required to dissolve
out the selenite.

3. The production of a salt which would entail a gradual destruc-
tion of the lamellar structure of the selenite, and would bring the
mineral down to the level of solubility witnessed in gypsum, might
account for the empty spaces. The theory which appears to be most
reasonable is partly that by which Bischof accounts for the decom-
position of beds of gypsum, and the consequent formation of other
beds of gypsum out of strata of carbonate of lime. Bischof may be
thus quoted* :—“ If gypsum is impregnated with organic substances
(bitumen) and comes in contact with water, it will be gradually de-

* Op. cit. vol. tp. 419.

VOL. XXII.—PART I. Cc

18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 22,

composed into sulphuret of calcium, while carbonic acid will at the
same time be formed. Should the carbonic acid pass from deeper to
higher strata, which are likewise undergoing decomposition, it gives
rise, in the presence of water, to a disengagement of sulphuretted
hydrogen, while the gypsum is converted into carbonate of lime. If
these exhalations of sulphuretted hydrogen become converted by
attraction of atmospheric oxygen into sulphuric acid, and this comes
in contact with the younger strata of limestone, gypsum will again
be formed.”

It may be noticed in support of the adaptation of this theory to
the cases under consideration, that the organic substances, some of
them even bituminous, were at hand, and that the clays were doubtless
always wet.

The former soluble condition of portions of the plant-beds may be
estimated from the blackening of the clay and loam immediately
around them; and it is probable that this solubility increased after
the deoxidation of the vegetable matter had been completed.

It is remarkable that the only trace of a sulphide in the portion of
the Woolwich beds under consideration, was found close to the sele-
nite impressions; and it is equally interesting in reference to the
theory I have adopted, that particles of selenite should have been
found close to the large moulds in the London Clay.

If sulphide of calcium was formed, as already noticed, and the
interlaminar spaces of the selenite were gradually the seat of its for-
mation, thus offering a large surface for its development and for the
action of percolating water, the gradual disappearance of the crystals
was but a matter of time. If these theories of the origin and removal
of selenite are correct, the decomposition of the plant-remains in one
case, and of other organisms in the other, were of equal importance ;
and it is from the abundance of the evidences of such decomposition
in the London Clay that the operation of solutions of organic matter
is inferred.

8. Conclusion.—The preservation of the impressions of selenite is
doubtless exceptional, and it is very probable that this mineral, like
many others, is formed, decomposed, and removed without any trace
being left of the complicated chemical operations which determined
its existence and decay. The existence of soluble salts in the Wool-
wich clay is remarkable, for they cannot be all derived from the per-
colating surface-water, but from the original constituents of the bed.
It is a proof of the great lapse of time required, even with the assist-
ance of alterations in the level and dip which determine increased
drainage, before such beds can be reduced to the mineralogical sim-
plicity illustrated by clay-slate.

The formation of gypsum, and of its more durable replacing erystal-
line form selenite, suggests the decomposition and destruction of or-
ganic remains, and the disappearance of these minerals is equivalent to
the destruction of the evidence of the former existence of organisms.

How organisms are preserved and destroyed in sedimentary strata,
are questions constantly before the geologist ; and these observations
have been made with the intention of correlating the disappearance

1865. ] FISHER—-CHILLESFORD BEDS. 19

of selenite with that of the organisms to whose former existence it
owed its origin. It is clear that if organisms deposited in sediment
contribute at the commencement to the formation of such minerals
as selenite, which are removeable in their turn, after a while the
sediment may become free from all trace of former organic matters.
In other words, there is no reason why the purest clay-slate may not
have been formed from a fossiliferous clay.

2. On the Rutation of the Norwice or FLuvio-Martne Cre to the
CHILLESFoRD Cray or Loam. By the Rev. O. Fisner, M.A.,

Durine the month of August last, in company with Professor
Liveing, I visited Orford and Aldborough, and we made some obser-
vations which may tend to clear up the uncertainty which hangs
over the relations of the Red Crag, Chillesford beds, and Fluvio-
marine or Norwich Crag. We took with us the paper by Mr. Prest-
wich on the Chillesford Beds, in vol. v. of the Society’s Journal,
that by Mr. 8. V. Wood, jun., “On the Red Crag and its Relation to
the Fluvio-marine Crag, and on the Drift of the Eastern Counties)”
(Annals and Mag. of Nat. Hist., March 1864), and the same author’s
“Map of the Upper Tertiaries of the Eastern Counties, with remarks
thereon,” privately printed, 1865. After having begun to digest
the materials we had collected, I visited the same neighbourhood
again in the beginning of September.

Mr. Prestwich has left it open as to “whether the Chillesford
deposit may not be identical with the Mammaliferous Crag of Nor-
wich”’*, or whether it ‘‘ may not belong to a period one stage more
recent than the Mammaliferous Crag ; whether in fact it may not be
the marine representative of that thin marine, freshwater, and land
series, which, on the north-eastern coast of Norfolk, is spread over
the patches of the Norwich Crag, and immediately underlies the great
northern clay drift,” 2. ¢., I conclude, Mr. Gunn’s “ laminated beds.”
Sir Charles Lyell, however, in his work on the Antiquity of Man,
decidedly adopts the former view, saying that “the most southern
point to which the marine beds of the Norwich Crag have been
traced is Chillesford, near Woodbridge in Suffolk” +.

Mr. Wood, jun., on the other hand, considers the Chillesford beds
to be a local member of the division of the glacial series, which in his
last-mentioned paper he terms “the middle drift.” He says, p. 4,
“The Chillesford beds described by Mr. Prestwich in 1849 as over-
lying the Red and Coralline Crags, pass up without the least break
into the middle drift, and are evidently part of that division.”? And
with respect to the Fluvio-marine Crag and its relation to the Chil-
lesford beds, he says, ‘‘The conclusion I have formed is that the
Fluvio-marine Crag of Thorpe is inferior to the fifth stage Red Crag”’
(that is, the phosphatic nodule bed), while in another place he states

* Quart. Journ. Geol. Soc. vol. v. p. 351. { Hd. 1863, p. 211.
c2

20 PROCEEDINGS OF THE GROLOGICAL SOCIETY. [Nov. 22,

that “this horizontal Crag” (2. e. the phosphatic nodule bed) “ passes
up into the Chillesford beds at Chillesford.”’

In short, Mr. Wood’s views, as he informs me, are these, “ That
the Red and Fluvio-marine Crag are coeval; while the Chillesford
beds are but a fossiliferous (and that only local) horizon of the
“middle drift,” at about one-third to one-half of the distance from
the base of that deposit, the horizontal crag being only the very
base of the ‘ middle drift’ over parts of the Red Crag area.”

I feel that any contribution towards the solution of this interesting
though limited problem is worth recording, and I can assure the
Society that my companion and I made our first examination with
no previous bias towards one view rather than another.

The section at Chillesford loam-pit close to the chancel of the

church gives— fe 2
Drift from the Boulder-clay. 3. .4 5%... 2.242 eee 5
Brown laminated loam with crushed shells .......... 2
Macaceous brown sand ii. it ae oS. eee ff

Light-brown sand with Mye in their natural burrows 0 6
Coarse sands, less micaceous, and not laminated.

In the adjoining pit of Red Crag, distant about fifty-eight yards,
there is a difference in character between the upper and lower half
of the section. The lower has the ordinary aspect of Red Crag, but
the upper appears to be a continuation of the sands of the loam-pit.

There is in the upper part a bed of shells horizontally stratified,
a foot thick at about 5 feet below the level of the Mya-bed in the
loam-pit. Then succeed 5 feet more of horizontally drifted shelly
sand, which rests on the ordinary obliquely laminated Red Crag.

Proceeding to Chillesford brick-pit, the loamy clay is dug for
15 feet, down to a shelly sand, but I did not meet with Mye in it.
In other respects the deposit agrees very closely in character with that
in the pit behind the church. In these two pits the grey colour so
characteristic of this bed at some points is only observable in a few
thin layers, the prevailing colour here being a light brown.

The same clay, of a greyish-brown colour, and resting on yellowish
sands, is met with in a clay-pit atthe western corner of Sudbourn
Park. The porous character of the sands is shown by the fact that
a field-drain, yielding a continuous stream of water, is turned into
the pit, and sinks away without forming any pool. The substratum
at this place must be Coralline Crag, which comes to the surface just
inside the park.

Thus far these Chillesford beds appear to consist of laminated
micaceous clays, sometimes brown and sometimes grey, having at
their base a sandy band, at some spots containing Myc truncate in
their natural burrows, the whole resting on a loose yellowish-brown
sand. These beds indiscriminately overlie the Red and Coralline
Crags. We found these beds again more or less modified between
Aldborough and the pit at Thorpe, near Aldborough, where the Fluvio-
marine Crag appears. There were indications at that spot which
appeared to us to show that the Chillesford beds pass under this Crag,
and I commenced the present paper upon the data we had so far

1865. ] FISHER—CHILLESFORD BEDS.

gathered; but not being satisfied with my
proofs, I determined to make a careful section
from Orford to the Thorpe pit, and at my
second visit walked over the ground for this
purpose.

To some extent the section will explain.
itself, but I desire to advert to a few parti-
culars of it.

The chief difficulty in the geology of this
neighbourhood arises from the repeated ero-
sions which the surface has undergone, the
newer beds being thrown down upon the eroded
surfaces of the older.

One consequence of this is that we ordinarily
find the succession incomplete. Another is
that any given deposit does not continue of a
uniform thickness, but while its upper surface, ——
where it has escaped erosion, is nearly hori-
zontal, the lower follows the contour of the
surfaces of the rocks on which it rests.

Another difficulty arises from the sandy beds
of the district being so similar to one another,
that it is difficult to distinguish them by their
lithological features.

As far as my notice extended I did not see
any indication of faulting, and the dip of the
beds appeared very regular, being very slightly
towards the north.

The section commences at the Orford wind-
mill, which is marked on the Ordnance Map
as being 54 feet above the sea-level. Here
the beds are capped by a drift gravel 7 feet
thick. It contains large flints and quartz ——
boulders, eight or ten pounds in weight. It
rests on the Chillesford Clay.

The clay or loam is seen in a small pit Ss
beyond Queen Esther Grove. It is exposed ©

‘[OAVIS-JJIIGE “D

‘BVIC OULIVUI-OTALT.T “9

‘poq-eAT “p

‘mRoTy 10 LeTO paxojsoT[IO ‘2

(eo) gL
for 10 feet, and rests on reddish-yellow shelly 3,5.
sand. At the interval of one field the shelly 3°
sand is seen beneath the hedge. A quarter OB
of a mile further on, at Sudbourn Church g ~
Walks, is a shallow pit in brown micaceous © 4
loam. The shelly sand, always more or less >
noticeable below the Chillesford loam, is well =

exposed in the bottom of this pit. A small
excavation which I made disclosed the Mya-
bed in great perfection. It was about 2 feet
thick, with three or four tiers of the united bi-
valves. They lay so close together that it was
impossible to remove one without breaking

“YSIB IAL

ye

Sudbourn

(Hist) ----. « Church
BAY,

a7) i =<

) Walks.

— see—= Sydbourn.

hw ee ok

purl
poyeajnoug

SEES Marsh.
sabe ieee River Alde.

Aldborough

\. eee town brick-

field.

Aldborough

|) -----~ old brick-

iln.

Thorpe _

-ybnosogpyy unou ‘adsoy JF 07 pLofug wouf woyssg—'| “Sty

22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 22,

others; but, from the fact of the matrix in which they were im-
bedded being harder than the sand which filled the shells, I found it
impossible to obtain perfect specimens. The upper part of this fossil
bed abounded in Mactra ovalis, a few having the valves united,
while the lower part yielded great numbers of Tellina obliqua, many
of which also had their valves united. The species which I collected
here were—

Trophon antiquum. Mactra ovalis (abundant).
Turritella communis. Tellina obliqua (abundant).
Mytilus edulis. Mya truncata (abundant).
Modiola modiolus.

Between this pit and Sudbourn Church loose sands occur. These
appear to crop out from beneath the Mya-bed.

At the bottom of the valley the Coralline Crag may be seen in a
pond, and several pits have been worked in that stratum on the side
of the adjoining hill. But there is one remarkable pit near the top
of the hill, due north of # in Ow Covert, which is referred to by Mr.
Prestwich in his list as consisting of Coralline Crag capped with the
Red Crag, and which appears to deserve description.

The overlying deposit, 15 feet thick, I believe to be riot Red Crag,
but a shoal-deposit derived from the Mya-bed. The appearance of
the deposit differs considerably in colour and texture from the un-
doubted Red Crag of Butley and Chillesford, the nearest points at
which I saw it; and while many of the commoner shells of the Red
Crag are at this place rare or altogether absent, those of the Mya-
bed are in profusion; above all Mactra ovalis, the common shell
hereabouts of the upper part of the Mya-bed, forms its chief ingre-
dient. ‘The Coralline Crag at this spot attains a higher level than
usual, which I doubt not was the cause of this remarkable accumu-
lation of dead shells, washed together during the formation of the
Mya-bed. ‘The species which I noticed in this crag were—

Mactra ovalis (in extreme profusion). Mya truncata (equally abundant).
Tellina obliqua (extremely abundant), Mytilus edulis (common).
preetenuis (abundant). Trophon antiquum (rare).

There is a resemblance between the species of this bed and of
that already described as occurring in the upper part of the Chilles-
ford Red-Crag pit, at a level a little below the Mya-bed.

Crossing the hill, the Chillesford loam is seen near a farm-house,
and the sands beneath it in the side of a lane near the bottom of
the hill. The Coralline Crag is dug in an adjoining pit.

Crossing the valley, I met with a bed of sand covering Coralline
Crag, the surface of which was eroded into hummocks. The place
is on the same line of country as the pit mentioned by Mr. Prest-
wich on the north of Ferry Farm-house, where he saw the surface
of the Crag “strongly indented by drift sands and gravel.”

This sand appeared to differ from that which I had hitherto
noticed as underlying the Mya-bed, and which I had just seen on
the opposite side of the valley. It contained a few flints of con-
siderable size, and the herbage which covered it was chiefly heath.

1865. ] FISHER—CHILLESFORD BEDS. 23

I have coloured it on my section as belonging to the sands between
the Boulder-clay and the Crag, whose geological position appears as
yet not well made out.

The line of section here crosses the hill obliquely. The Chilles-
ford Clay was seen near the top of it, by the side of the road. At
the extreme end of the hill, where it sinks beneath the marsh, sands
were seen which I believe to be those underlying the Chillesford
Clay.

Bing the marsh, the section enters a low cliff towards the
River Alde, close to the Aldborough Gas-works. This cliff is com-
posed of drifted sands containing frequent small patches of shells.
There is one rather constant band of shells about 11 feet from the
base of the cliff. It is best seen in a pit by the side of a lane oppo-
site the Gas-works. The-shells found in the cliff were—

Tellina pretenuis (very abundant). Cyprina Islandica.
obliqua (abundant). Mactra ovalis.
Mytilus edulis. Cardium edule.

Mya truncata.

At 5 or 6 feet above this band of shells, at the top of the low
cliff, the Chillesford Clay commences. It is extensively worked at a
brick-pit between the cliff and Aldborough Church. The clay is
capped by brown sands.

The Mya-bed is not seen at this spot, but close to the first mile-
stone from Aldborough it appears in the roadside-cutting. The
species collected there with scarcely any searching were—

* Tellina obliqua (valves united) Turritella communis.
Mya truncata. Natica.
Mactra ovalis. , Calyptreea.

Buccinum undatum.

The lower ground hereabouts is occupied by the Coralline Crag, which
is exposed in a large pit just on the west side of the line of section.
Mr. Wood noticed in the heading of this pit at one place traces of a
shelly crag, and at another a patch of phosphatic nodules. We saw
also both these. They appeared to have been drifted; and I have
little doubt that the Crag had been derived from the Mya-bed, and I
think it very possible that the nodules may have come from the Coral-
line Crag itself. We found such in the Coralline Crag at Sudbourn
Park, which renders it not unlikely that an old water-washed sur-
face of that rock might yield them.

The Chillesford Clay is again met with in the Old Aldborough
brick-kiln on the rising ground above the Crag-pit. This is the
brick-kiln mentioned by Mr. Wood.

The clay is here overlain unconformably by brown sands.

A tract of low marshy land is now crossed, upon which we saw
traces of Coralline Crag, as we thought, dug out of a deep hole.

The rising ground beyond the marsh, on which to the east stands
the hamlet of Thorpe, consists of brown sands. They are rather
coarse, and contain ferruginous layers. These sands are exposed
in a railway-cutting on the edge of the marsh. A little further

24 PROCEEDINGS OF THE GEOLOGICAL socieTy. [Nov. 22,

on, about a furlong and a half beyond a crossing over the rail-
way, there is a small sand-pit. Its position may be found on the
Ordnance Map on the side of the hill opposite the last h im “‘ Ald-
ringham Church.” Here we met with an abundance of impressions
of shells in the more clayey layers. The most common species was
Mytilus edulis. The shells (as well as I can distinguish them) appear
to be—

| Mytilus edulis (abundant). Pecten. Cardium.

Two furlongs further to the north is an old pit overgrown with
herbage. It is in brown sand. Near it is another of similar ma-
terial with water in it; and a few yards further to the north the
Thorpe “ shell-pit” is reached. This has been considered, I believe
rightly, to be an exposure of the Fluvio-marine or Norwich Crag*.
Its thickness is very considerable, but owing to the state of the pit
it is not possible to estimate it exactly +. It must, however, attain
ten or twelve feet in the pit. There is also a trace of the same bed
in the bank on the western side at the end of the lane near the n
in “ Aldringham Common.” This must be 30 feet or more above
the bottom of the pit, though it does not necessarily follow that the
deposit was that thickness; nor am I positive that it is am setu.

At the bottom of the “ shell-pit” is a small pool of water, and
digging at its edge I soon reached the bottom of the bed of Crag.
In its lowest layer were numerous pebbles of indurated brown
micaceous sandy clay, and beneath it the brown sandy clay itself,
from which they had evidently been derived.

A strong spring rose from the junction as I dug, and I have no
doubt it is the same spring which supplies the small pond resting on
brown sandy loam, already mentioned as being close at hand.

We were impressed with the opinion that we here had the Fluvio-
marine, or Norwich Crag, resting upon the Chillesford Clay. Before
my second visit to the place it occurred to me that this Crag might
be a drifted condition of the Mya-bed, as I believe the fifteen feet of
shelly Crag resting on Coralline Crag near Ferry-farm to be.. But on
examining the evidence again I was confirmed in my former opinion.

I have mentioned brown sands as covering the Chillesford Clay at
both the Aldborough brick-pits, and as appearing again between the
marsh (through which flows the Hundred River) and the shell-pit.
These sands are, as I have stated, fossiliferous in the latter place.
They may be seen, emerging from beneath the Boulder-clay, at
Aldringham Green, ‘and they are again capped by it just north of the

* Woodward, Phil. Mag. 1835, p. 354. Gunn’s Geology of Norfolk, p. 12.
Wood on Red Crag. Ann. & Mag. Nat. Hist. March 1864, p. 9.
+ The species I found here were—

Buccinum undatum (abundant). Tellina es
Purpura lapillus. —— lata?

Litorina litorea (abundant). -—— pretenuis.
Conovulus pyramidalis. Mactra solida.
Cerithium tricinctum. Cardium edule.
Turritella communis. Cyprina Islandica.
Pecten opercularis. Mya arenaria ?

Mytilus edulis.

1865. ] FISHER—CHILLESFORD BEDS. 25

village of Thorpe. The spread of these sands generally obscures the
subjacent rocks, but by a valley-denudation the Norwich Crag is
exposed at the one spot described; and I believe the top of the
Chillesford Clay to be also exposed for a short distance. To the
presence of this clay I attribute the water which is found in the pit
close by the shell-pit. The sands would not support water.

The stratification of the district strongly favours the view I have
taken of the superposition of the Norwich Crag upon the Chillesford
Clay. On the other hand, it would be quite possible to conceive
that the Mya-bed might be here expanded into a thick bed of Crag,
and this is what has been generally assumed to be the case. I
think, however, that the evidence rather supports my suggestion.

In the first place, the assemblage of species as seen at the shell-
pit differs from that of the Mya-bed. As strongly as I felt convinced
on the spot that the Crag above Ferry-farm was derived from the
Mya-bed, so strongly did I feel that the Crag at Thorpe was not de-
rived from it.

In the second place, the pebbles of indurated clay found at the
bottom of the shell-pit exactly correspond in composition and colour
with the Chillesford Clay, wherever it is weathered brown, as, for
instance, at Chillesford itself.

In the third place, I have always noticed a porous sand under-
lying the Mya-bed, which would not support water. Indeed, in the
clay pit near Sudbourn Park I have mentioned that a run of water
from a field-drain is conducted to this sand and immediately lost in
it. If, therefore, the Thorpe Crag were on the horizon of the Mya-
bed, I do not think that we should have a spring at its base, nor a
pond close by in the subjacent stratum.

The conclusion then appears to be correct, that the Fluvio-marine
Crag at Thorpe near Aldborough rests on the Chillesford Clay, and
that the descending sequence in that district is—

1. Fluvio-marine or Norwich Crag.

2. Chillesford Clay. 3

3. Mya-bed resting on sands, which, as at Aldborough Gas-
works, are occasionally fossiliferous.

4, Red Crag.

Let us now see whether this sequence is borne out by other expo-
sures of these beds. |

It has long been known that a formation containing, as Sir
Charles Lyell tells us, “lamellibranchiate shells with their valves
united, mixed with land and freshwater Testacea, and with the
bones and teeth of Elephant, Rhinoceros, Horse, and Deer” *, occurs

* Hlements, 1855, p. 156. Since this paper was read I have been favoured
with the sight of a letter written in 1864 by Col. Alexander to Mr. Searles V.
Wood. Putting the contents of this letter by the side of the information I have
received from Mr. Ewen, I gather that four Mastodon teeth have been obtained
on this coast. That which is figured by Professor Owen in his ‘ Fossil Mammals’
was found on the beach at Sizewell Gap, near Thorpe. Another, which Mr.
Ewen now possesses, was found under the cliff after a fall at Easton Bavent.
A third, with part of the jaw attached, was seen by Col. Alexander in the talus

[Nov. 22,

26 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

at Easton Bavent Cliff near Southwold. I visited this spot in
October, and was at once convinced, by the identity of the lithological
character, that we here have the Chillesford Clay underlain by the
Mya-bed.

Yet at this spot, as at Chillesford Brick-pit, I found no Myas zn
situ, though single valves occur. Tellina lata, with its valves
united, is extremely common, as is also Tellina pretenuis.

- Immediately beneath the Chillesford Clay we come upon a band of
drifted shells, two or three inches thick, containing flints and frag-
ments of bone imbedded in a coarse sand, and, beneath this, sand
with Telling as they lived. The bed occurs, where I saw it, at the
very bottom of the second cliff north of the farm-house, and was
only visible for a few feet, the rest being obscured by talus.

The following species occur at this spot :—

Tellina lata. Mactra ovalis.
obliqua. Pecten opercularis.
preetenuis. Cyprina Islandica.

Mya truncata. Litorina litorea.

Leda myalis. Paludina lenta.

Mr. Ewen of Southwold, a friend of the late Col. Alexander, in-
formed me that this band used to occur twenty-five years ago higher
up in the cliff, and to the south of the spot where I found it, but
that it had, through the wasting of the cliff, descended beneath the
beach at the old locality, owing to the dip of the bed. This is im-
portant for my theory, as will appear in the sequel.

On examining other spots in the neighbourhood of Southwold, I
found a pit at a place called Yarn Hill, near Potter’s Bridge. Here
is a bed of shells, chiefly Teline in sand. It is covered by a brown
loam, which I believe to be weathered Chillesford Clay, a band of
flints in sand intervening; I have no doubt of its being a continua-
tion of the Mya-bed seen in the cliff.

The species found at Yarn Hill were :—

Tellina obliqua (common).
lata (common).
preetenuis (common).
Mactra subtruncata (common).
ovalis (not common).
Cardium edule (common).
Cyprina Islandica (fragments).
Mytilus edulis.

Litorina litorea.
Buccinum undatum.
Natica catena.
Guillemini.
Ringicula buccinea.
Paludina lenta.
Succinea oblonga.

On the hills above this pit are pits of Chillesford loam and clay,
extensive brick-works being carried on in the latter at Manor House,
Frostenden, and other places. At Frostenden brick-kiln the sand is
dry beneath the clay, but the Mya-bed appears to be absent. Draw-

of the same cliff, and appears to have come from some position above the Mya-
bed. It fell to pieces. A fourth, now in the possession of Mr. Ewen, was taken
from the Mya-bed. It is the tooth of a very young animal.

Col. Alexander speaks of the occurrence of Crag shells in the talus of Easton
Cliff to the south of the outcrop of the Mya-bed. ‘The impression left on my
mind is that some patches of Norwich Crag were then existing in the cliff in the
position I have assigned to it above the Chillesford Clay, but hidden by talus.

1865. ] FISHER——CHILLESFORD BEDS. ail

ing a line from the spot where the Mya-bed occurs on the beach to
the pit at Yarn Hill, which is scarcely raised above the sea-level, and
bearing in mind that the outcrop on the coast has been carried be-
neath the beach towards the south by the encroachment of the sea,
we obtain a dip towards the south-west.

Proceeding to Wangford, we meet with pits in the true Norwich
Crag, exactly resembling the deposit at Thorpe, near Aldborough, and
at the pits about Norwich. It is a gravelly deposit of considerable
thickness ; how thick the section does not show, because the upper
part is denuded, but about 9 feet remains. The shells are not grouped
as in the Mya-bed, the proportion of univalves being greater. None
of the bivalves are in pairs. Here I found an antler of a deer, but
too much decayed for removal.

I dug in the floor of this pit and found the Crag to rest on a lami-
nated sandy loam, closely agreeing with the upper part of the Chil-
lesford Clay at Easton Bavent Cliff. The dip of the beds to the south-
west, as determined above, agrees well with this identification.

There is another pit, which I had not time to visit, at Bulcham
Workhouse. I am told by Mr. Wood, jun., that it is in the Norwich
Crag. Its position would agree very well with the view I take of its
superposition on the Chillesford Clay.

Thus the observations I was enabled to make in the neighbourhood
of Southwold confirm my former view, that the descending order of
sequence 1s—

1. Norwich Crag,
2. Chillesford Clay,
3. Mya-bed;

while they give the additional fact that the Mastodon and other
Mammalia have been procured from the Mya-bed at Easton Cliff.
We cannot, then, hesitate to include the Chillesford Clay in the Nor-
wich Crag series.

I am not aware whether the Chillesford Clay occurs in the Norfolk
district of the Crag, where it rests immediately upon the Chalk.

There can be no doubt about the Chillesford Clay being a marine
deposit, for I found in it a lenticular patch of sand containing shells
similar to those of the Mya-bed; and Mr. Prestwich and Mr. Wood
found marine shells in it at Chillesford. The character of the deposit
might otherwise have led one to suppose that it was lacustrine.

There are still some problems of considerable complexity to be
solved respecting the sequence between the Mya-bed and the Red
Crag, and again from the Norwich Crag upwards.

It is well known that in the district of the Red Crag there are
thick beds of reddish-brown sand overlying the fossiliferous Red
Crag. These have been called “ the unproductive sands of the Crag’’*.
Mr. Wood, jun., considers them to belong to his “ middle drift,’”’ and
thinks that the Chillesford beds are a local modification of them. I
am not prepared to deny that the Chillesford beds, and therefore also
the Norwich Crag, may be a local modification of these sands; but I

* Prestwich, Quart. Journ. Geol. Soc. vol. x. p. 93, note.

28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 22.

question their bearing any relation to the sands which usually underlie
the Boulder-clay, and which Mr. Wood has called “ middle drift.”
Indeed, I believe that he feels that difficulty himself, for he is unable
to make a separation between these unproductive sands and the
phosphatic nodule-band, and yet he evidently shrinks from dissoci-
ating that peculiar band from the general deposit of the Red Crag.
He says, ‘‘I incline strongly to a belief that this horizontal Crag is
merely the redeposit of the material of the Red Crag beach, washed
up on the submergence of the Crag beneath the middle-drift sea ;”
though further on he adds, “ but in the case of the horizontal Crag or
nodule-band, this dissociation” —of the nodule-band from the Red
Crag—* seems difficult to arrive at”*.

My own impression is that the mass of sands met with between
the Boulder-clay and the Red Crag belongs to several deposits of
different ages. The unproductive sands of the Crag, which are of a
peculiar unctuous character, are one deposit. The laminated brown
and yellow sands seen, = instance, about Aldringham Common,
in which I found Myili abundant, are another, and I suspect belong
to the “laminated beds” of Mr. Gunn, which underlie the Norfolk
Till. We have still a third deposit of sand in the “ middle drift,”
overlying these, and containing those beds of rounded pebbles which
have contributed chiefly to form the beach of the Suffolk coast.

I believe that all these sands may be seen emerging from beneath
the Boulder-clay in the interval between Westerfield and Bealings
stations on the East Suffolk railway.

* Remarks, &c., pp. 5 & 6.

PROCEEDINGS
OF

THE GEOLOGICAL SOCIETY.

POSTPONED PAPER.

On the Carsontrerovs Rocxs of the Vautey of Kasumere. By
Capt. H. Gopwin-Avsten. With Nores on the Bracuiopopa col-
lected by Capt. Gopwin-AvstTEN in TurBet and Kasumerg, by T.
Davinson, Esq., F.R.S., F.G.S.

[Communicated by R. A. C. Godwin-Austen, Esq., F.R.S., For. Sec. G. 8]
(Read partly on May 25, 1864, and partly on June 21, 1865*.)

THE district or Pergunah of Vihi is situated on the right bank of
the Jhelum, above Srinagar, and is bounded on the N.W. by Ze-
banwan (8813 feet), on the S.E. by Wasterwan.

The rough panoramic sketch (fig. 2) of the hills which surround
this valley, as seen from the line of the river looking east, indicate
the positions of the several places at which the following sections
were taken. The distance from Zéwan to Reshpur is about 8 miles.
The level plain consists of the lacustrine and alluvial deposits of the
Kashmere valley, through which the streams from the hills have
eut deep courses. The Jhelum flows between high banks of the
same formation.

Everywhere, both in Kashmere and Thibet, a Paleozoic series
underlies the Mesozoic formations. The age of the Paleozoic rocks
is that of the Carboniferous series of Europe, but as yet fossils have
not occurred to enable me to distinguish any formations of older
date. As, however, Lower Silurian fossils from the Khyber Hills
were found by Dr. Falconer in the gravel of the Cabul River, as
also by Colonel Strachey on the Niti Pass, the great masses of slaty
and metamorphosed rocks, which in this part of the Himalayan chain
underlie the Carboniferous beds, may be referred to a Lower Pale-
OzOi¢c series.

The Carboniferous formation may be traced all along the range of
mountains on the north side of the Kashmere valley, where, in con-
junction with Dr. Vercher, I met with its characteristic fossils in
great abundance.

Fig. 3 is a section along a spur from Wastesmau: between Barus
and Reshpur, in a direction from 8. to N. At the base are the
metamorphosed hornblende-slates of Wasterwan Peak. Next comes
the quartz-rock, followed by beds of limestone (fig. 3, p. 31).

_ Beyond Zéwan, to the east, near Khoonmoo, is an outlying or
projecting ae of limestone(fig. 4); the strike is 8.W. N.E., and the

dip. 30° S.E
* For the abstracts of these communications already published, and for the

other communications read at these evening-meetings, see Quart. Journ. oie
Soe. vol. xx. p. 383, and vol. xxi. p. 492.

30

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Fig. 1.—Sketch-map of the District of Vehe.

hea! 4
Bi det
AGAR ro

ae

coed),

62687,
LMU !

Es
fe PHN,

(Sul

ee

la
=| (Fi,
Se (Yi
SVAY
ESS S
ENS
ZS ys
aN =
Cie XY
1A
4 Noe

se

\

4 sa SKBAN ADAM

Tos eS
\ FY yp WON.
es Mion lly

a\(,

117 ey

'
\

Was

i]

\

Ngee

OHM

“4, Wi,

hihi

yi

4 ABYGYY YY

Cerman

1

We ews
A

SS =<
VAS AYRES
an i Ns ae

i i

SY,
SS

4 =

Mie
Inet

Ui

The dotted line at the base of the hills indicates the boundary of the lacustrine
formation.

31

GODWIN-AUSTEN—KASHMERE CARBONIFEROUS ROCKS.

0¢6 *OUOJSOULTT JO SHV, ‘yoloay vaafiudgy—s|[oys pordosord-]joa Jo [TMF pueg °C
—- “foT[Ba orourysey oy} Jo Avpo TeLanT[Ty “6 ‘euoysoumty Apues snosovory, “GC
OOT eevee re once 9.100 QUST] SUTIOY}VOM ‘QUOSOUIT] goed ut00 prey To) Cl ee ec cc escr ec eerste eres es ve ce ec ee ee ese pueq Ayers a
OIF eoseeeee LF STISSOT OU—9U0}SoUIT goed 109 pilex ) COL “3 ‘F peq pue , ‘Sy ‘e peg)
Os. SS UMOAG JUST ‘syoor poroyzeom ‘ouoysoumty Lory “9g OF (spoq WeANZ) S[ISSOF JO [[NF ‘Moers SuTTOYyVeM ‘ouoysounr] ATeYG °*g
69... ae ere [[@ UI—speq esey} usemyoq Joot GE ynogy 08 °' SPoq TOMOT SP1BALO7 OS SSOT { OUOIOUATT SNOAOJITISSOF PALF] °G

; "SNIDINIUALUMAS SNZINPO gta ‘oC, 2G Ci ec ctece eer eeeseerce ee cree or ee ee ee ee yoo zyxenb opty A. a
400} "400F

@ Soe 1s 9 .
UY HY |) Ss ey Ds ae
TH) 7. Pi ies
PLENTY WS pes Wf
EAH L (— f= U Ht
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oN LY
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: = aie il) 4
= ‘ Ll) VY}

‘roodyuvay pur snseg 07 ndysey wory peoy
‘undysaay pun snung woomjag “unmagsny woul inds v buopp uoysg—eE ‘Sq

“TLOTJRUIAOF OUTAJSNOR] OY} JO ArepuMog oY} SoJBOIPUT S][IY oy} JO oseq Oy 4B OUT] Po}op oy,
‘snieq °9 ‘ndysoyy *G ‘oopoorT ° ‘uekIBAA "S ‘OOMLUOOY YY *G "TeMULGIZ IO UCMEZ °T

= <>

LALIT Tee a + =
- a SFE 2 ee eee ae 5 = =e

cs Yd GUM We. Ree eee ee en eee - Se
VG, 4 \ eee See a ee —-—~ = Sad —————__—
dy Le Le aes i ————— are
Boe

~ : vor a af ee —— -
| ‘auamysny ‘hayoy wera 2Y) punow spy ayn fo yopoyy ovupsoung ybnoy—z *B1q

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Fig. 4.—Section near Khoonmoo.

PS zi are

Was

4, CD eS SSS &y § 2 Sais
The upper part of the bed next above the Hornblendic rocks and

slates is

feet
I. Fime compactirock-——caleareous J... 225+ -5--0- <> 05 eee
2. Light purple sandstone, with particles of hornblende................ +)
o. Hard dark-blue'slatesalternatimg withis. (5). 2. a. «2. «1-/)s)15 eaten 2
4. Brown shales and hard sandstone 7)... a... t= oe 15
5. Black limestone (like the marble pillars of the Shalimar Summer-house) 4
6. Shaly limestone.

No fossils were found in any of these beds.
Fig. 5 is a section across an outlier of limestone at the foot .

of a ridge from Zebanwan to the S.E. Thestrike hereisS.W. N.E.,
dip 30° S.E.

Fig. 5.—Section at the foot of a ridge, from Zebanwan, to the 8.K.
N.W. S.E.

cst a eee Me Ore . N WN

6.—Plan of the ridge near Zebanwan.

/ Ne Mi

GODWIN-AUSTEN—-KASHMERE CARBONIFEROUS ROCKS. oo

On the hornblendie slaty rock, which here everywhere underlies
the Carboniferous series, there is in ascending order—

feet.
en Re Se TIGY CMALTZILO (5 bole! 5 oss aise sg SHER Bate nak wahelonslyecay aalaalele 12
Passing up into
. Altered sandstone and shaly beds, very hard and splintery .. 15

2
3. A bed of water-worn pebbles and shingle, of quartz and hornblendic
reck, imbedded ina sandy crumbling matrix ...........065 0000s
The shingle at the bottom is much the coarsest.

. Sandstone, also containing water-worn pebbles .:..............0065 2
Pamermations of shaly, slate and sands... 6s... cece eee ce ee agtee ee 30
Bee See O IB SAGs eLnie soa ie teas gH Mine ct a\ste en tile ae eee gfee vee 20

Passing. up into
. Hard compact crystalline limestone, of a dark-blue grey, interstratified
with grey shales, which weather to a green tint.

NI HOoPF

Both the limestones and shales are extremely fossiliferous, con-
taining many Brachiopoda. I have given this part of the series
(Nos. 6 & 7) the name of the Zéwan beds, from the village near.

The section (fig. 7) near Barus, on the right bank of the Jhelum
River, Kashmere, under Wasterwan Peak, exhibits the following
strata, having a-dip of 50° W.

Fig. 7.—Section on the right bank of the Jhelum River, near Barus.
Road. ae

IPR RN Eee ose BO oa ofa dl ough np areata, site vw ohays <:hi a Sn bya eh oa 20
2. Hard compact limestone, Pedderus scabriculus, Ter. sacculus, Athyris
SN ee CS i Pe i Sie aillwiaht Sz dunit 2 he « We euabakel
3. Shaly limestone, full of Fenestella, Streptorhynchus crenistria. Zewan
DE ei caren once: ote ce inn sag aa, Mek ase RUMEN Sones as ieee 50
‘Spirifer Moosakailensis, Day., and Productus semireticulatus.
4. Compact limestone, with few and obscure fossils ......0.....-05. ... 100
m@aleareour slate or shale .... 2... 2625 ee emcee eens es A re ERS he. ted 30
6. Micaceous sandy calcareous beds—in all... 1.1... 62. e ce cece ee eee 60
6a. Spirifera Rajah. ye
66. Productus semireticulatus, P. scabriculus (large form), Chonetes
levis, C. Austeniana, in great number.
30 feet between. Beds 5, fig. 3.
7. Hard compact grey limestones. No fossils seen, about.............. 150

Section across the Entrance of Ravine.*—Above the village of
Khoonmoo there is a very interesting section, as a great thickness of
the Carboniferous series is exhibited. On the left, and overlying the
Hornblende-slate series, are the beds represented in Sect. B, dipping
in the same direction as all the other beds at this place.

* A large Chunar tree stands at the entrance into the ravine.
VOL. XXII,—PART I. | D

34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Fig. 8.—Plan of part of the district on the right bank of the
Jhelum River, near Barus.

Fig. 9.—Section across the entrance of the Ravine above the Village
of Khoonmoo.

}., Compact quartzite scsi akicloe cleretiats a bes pole cue ee OC 12
2. Sandy calcareous beds, with a few shells ............0..0cceeeece 10
3. J#ard limestone, with Orthoceras .....<.....<<«+s+s- nse Sere 10
4, Limestone, with small Productus scabriculus, Spirifera Kashniriana,

IS AU VON as iin aiaisttacne Sige the & iphesv eos Gere ae peels tunias tee 3
B. Gvey Limestone 5. 357.5" wa einen Some tee ciatere se eie. tis tia] e easter ea: eee ae ae 6
6. Bed with shells, &c., well preserved, Athyris subtilitd...... 02.0.0 ae 2

6a. Compact unfossiliferous limestone beds .............64, «+ «ie pa

65. Bed made up of broken Brachiopods ..............-.ssse05 20

7. Limestone up to the great fold of the beds, extending to the ridge
full 3500 feet above the valley, and including a bed containing
Bryozoa at the horizon indicated by the figure ................ 1200?

The valley above the Shalimar Garden lies over on the other side

ae, a! ¥
Why ; mc f ; ;
« i ae
a te Lie hhh re ts Oe Aa i
} i
{By At ph i ‘
‘ Malad, Pe :
/ /-
hi » x ‘ + a ie fa aes: ,
Raven (0 i A RR ok eA os?
? ¢ Ate ; bo ae ae } ;
pat ht % ; rie PP a ’ } 44 | ‘ / Tk ete, Ke
: . 4 . J “Y ‘ey 5
x ae hare at + ‘> A, 4 + oa y¥t.s ba Ass RIE IAT
ee iia a Oe
iyite ae
4
'
4
oe i
iit tegen paicivt 3 Waien
ema eT hen ila ony Ae orth. cacett & “Et et! ASRAL
ry: i Fe nae ay Sey cork yt rs o7 i ied Gt Ma My 8" » i 2 Pas Sait
ery it be -4 mire ; ‘Pr: y ot f
uige PPR TL og a) OEE ADRES AP Pe har ge eee
PA +s : , P
Ay A bids i tl big ah . i
F) 5 q ; :
SMA | t Aa 551) W45 %*
‘ r > .
Lh pb | Tt; i eh | j >
a! 7 eh D DAY d
My che { vy ry ‘ ‘ i
OT } hay ;
inst ; Pa} d
>> ‘Wehas . ices nen
: ee ay a ie Re: ‘ at ae
A >
v iY yar tie Ps dak ee © a of Sie . t
: a5 xy ; + ‘ he
/ 4
Pan
WY ote
re a
3 Bier
i
i
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vive a y

aed

[To face p. 35.

CorricgEenDA to the Axstract of Capt. Gopwin-Avstey’s Paper—
“‘GrotocicaL Norzs on Parr of the Norta-western Himatayas,”’
published in Quart. Journ. Geol. Soc. vol. xx. p. 383-387.

Page 385, line 29, erase the paragraph commencing As these lime-
stones, and ending Ladak and Little Thibet.

The Nummulitic series occurs, as has been stated at the com-
mencement of § 3, p. 385, line 27, on the southern face of the Pir-
Pinjal range and close to the older Siwalik rocks, but I have nowhere
seen it in the Kashmir valley, and I think it very probable that in
ancient days the Nummulitic sea conformed to the base of the pre-
sent line of Himalayahs, more or less, and did not extend to the
north at all. The limestone near the Wuller Lake, and at the base
of the hills on the northern side of the Kashmir valley is undoubt-
edly Carboniferous.

Page 385, line 12 from bottom, the paragraph commencing On the
southern slopes up to showing the palates very well, p. 386, line 2,
should have come into § 2. The Siwwalik Series; it not bemg Num-
mulitic, but the next formation in the series above.

5. The Carbonferous Series, p. 386, line 14.—It is a little
ambiguous, and might lead the reader to suppose that the genera
mentioned occurred indiscriminately through the whole mass of the
beds up to that and together with the bed containing Goniatites.
These, I may mention, contained no other shells that I could find.

I see it also stated —“ These also occur in superposition.” Now 1
should say hardly ever, and never in the Kashmir valley itself.
Further east, in Zauskar, Spiti, &c., the Palzeozoic and Mesozoic may
do, but not in the mountains to the south, south-east, and east of
the valley.

In Mr. Davidson’s note on the fossils, p. 387, line 20, it is
stated :—“<From this rock, at Shigar, near Skardo, Capt. Godwin-
Austen obtained six or seven, &c.” Now the fossils mentioned were —
all found in the Carboniferous limestones of the Kashmere,valley and
have no connexion with the very imperfect specimens, said to be Pa-
leozoic, obtained near Skardo. I am afraid the labels on the fossils
must have come off, or that by some means they got mixed together.
The same must have occurred to the land and freshwater shells sent
home; for Heliw hispida was obtained in the lacustrine clay of the
Kashmere valley, and not from Kuardo near Skardo. Some of the
other shells are from other localities, but as I have no duplicates I
cannot remember whence they came.

H, Gopwin-AvsTEN.

Deyrah Dhoon,
7th December, 1865.

DAVIDSON——THIBET BRACHIOPODA. 35

of the ridge, at the head of the ravine, in which valley I think that
the lowest beds will be found.

The section given in fig. 10 was taken on the south side of the Vihi
valley, near the village of Loodoo, across a ravine beneath Was-
terwan Peak.

Fig. 10.—Section on the south side of the Vihi Valley, near the
Village of Loodoo.

Above the usual basement-rocks, consisting of the Hornblendic
slate, of which a considerable thickness may here be seen, are
feet
1. Dark splintery slate and quartz-rock, with badly-defined lamination .. 20
2. Light olive-green splintery rock, very compact, fracture cuboidal, like 2

in fig. 5 Few ecw ce em ence renee cece tenes eect acne reer er scretres 2
3. Beautiful white or light-grey quartz, like flint .................0.005 1
4, Blue limestone, with beds which weather light-green ....... oO

This is bed 3 of fig. 3; contains the same species in great numbers.
The lower beds contain, or may be said to be made up of Fenestelle.
5. Dark-blue shales.
These shales occur in the opposite side of the ravine, and are sur-
mounted by a great mass of hard compact limestone (/), weathering
to a red tint, and containing Goniatites.

Note on some CaRBONIFEROUS, JuRAssic, and Cretaceous (?) BRAacHIo-
Popa, collected by Captain Gopwin-AUvstEN 2n the Musraxn HItts,
im Turpet. By Tuomas Davinson, Ksq., F.R.S., F.G.8.

(Puare I.)
§ 1. Carsonirerovs SPEcIES.

Tur Carboniferous series in Thibet is stated by Capt. Godwin-
Austen to consist of :—(1) quartzites ; (2) limestones full of fossils
of all kinds ; (3) an argillaceous series; (4) compact limestone with
fewer fossils, surmounted by a succession of beds full of Goniatites.
The impure limestone (no. 2) is of a darkish grey colour, and
appears in some parts to be a mass of organic remains ; it bears much
resemblance, both in the character of the rock and in its fossils, to
deposits of a similar age in Great Britain. From this rock at
Shigar, near Skardo, Capt. Godwin-Austen has procured six or seven
species of Brachiopoda, of which four only are determinable, the
remaining two or three being too imperfect to admit of a satisfactory
determination. |

1, Terepratuta AUSTENIANA, spec. nov. Pl. I. fig. 1.

Shell almost circular, nearly equally and moderately convex ; sur-

* Sect. C.
D

36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

face smooth. Beak moderately produced, and truncated by a small
foraminal aperture ; marginal line slightly curved in front, but not
affecting the regular convexity of the dorsal valve, while it produces
a small depression or sinus near the front of the ventral. Only one
specimen of this shell was found by Capt. Godwin-Austen in Thibet ;
it measures 1 inch in length and breadth, by 4 inch in depth.

2. Sprrirer, sp. PI. I. fig. 4.

Of this Spirifer, two fragments of the dorsal valve have been col-
lected ; when perfect it was semicircular, moderately convex, with a
smooth wide slightly raised mesial fold, each valve being orna-
mented by some twenty-eight or thirty flattened ribs. The ventral
valve being unknown, it would be unsafe to venture upon a specific de-
termination, especially as several Devonian and Carboniferous species

present characters very similar to those displayed by the fragment
under description.

3. RHYNCHONELLA PLEURODON, var. Davreuxtana, De Koninck.
Pl. I. figs. 2 & 3.

Several specimens agreeing with British and Belgian examples
of RL. Davreuxiana, De Koninck, have been found by Capt. Godwin-

Austen (see Davidson, ‘ Mon. British Carb. Brachiopoda,’ pl. 23.
figs. 19-21).

A, Orvis, sp. Pl. I. fig. 5.

Two fragments of one valve only were collected by Capt. Godwin-
Austen. In shape this valve is semicircular, with rounded cardinal
angles, 1 inch in length, by 1 inch 2 lines in breadth. It is mode-
rately convex and ornamented bynumerous fine radiating strie, which
increase in number by the interpolation of ribs at various distances
from the beak. The surface is likewise crossed by numerous con-
centric lines. These fragments are not, however, sufficiently com-
plete to warrant a specific determination.

5. Propuctus sEMIRETIcULATUS, Martin. PI. I. fig. 6.

Specimens of this characteristic Carboniferous hel do not appear
rare in the Thibet limestone.

6. CHonreres Harprensis, var. Turperensis. PI. I. fig. 7.

This small species occurs by millions in the Carboniferous lime-
stone and shale of Thibet, where it does not appear to have
much exceeded 44 lines in length and 7 in width. Prof. De Ko-
ninck agrees with me in considering it to be a variety of C.
Hardrensis. The shell is semicircular, concavo-convex, with a
straight hinge-line, each valve being provided with a narrow sub-
parallel area. The surface of each valve is ornamented with from
thirty-five to fifty rounded ribs, of which a small proportion are
due to interpolation. The surface is also traversed by fine con-
tiguous strie. As I have elsewhere observed, C. Hardrensis is a
very variable species, and this has, no doubt, induced paleontolo-

DAVIDSON——THIBET BRACHIOPODA. ol

gists to consider some of its local variations in shape as distinct
species. The strie vary much in number and strength; in some
British examples they are exceedingly numerous and fine, while in
other specimens they are much less numerous and coarser, the shell
differing in size much according to age and locality. C. variolata,
D’Orb., is, I believe, only a different name for the same shell.

§ 2. Jurassic SPEcrEs.

According to Capt. Godwin-Austen, rocks of the Jurassic period
are largely developed at Kato, in Ladak, in the Suru Country of
Thibet. In a limestone rock of a yellowish colour, which Capt.
Godwin-Austen refers to the Oxfordian period, the two following
species of Brachiopoda have been met with.

1. TrrepratuLa THIBETENSIS, spec. noy. Pl. I. figs. 11-14.

- Shell longer than wide, sometimes oval and rounded in front,
but more often truncated or indented at the front, and even bipli-
cated. Ventral valve regularly convex and rather deeper than the
‘opposite one; beak incurved and truncated by a circular foramen ;
dorsal valve evenly convex or biplicated near the front. Dimen-
sions variable. Length 1 inch 8 lines, width 1 inch 1 line, depth
11 lines.

This species is extremely variable in its external shape, so much
so, indeed, that were I not provided with thirty-five or thirty-six
examples, showing every intermediate form, I should hardly ven-
ture to consider them all as variations in shape of a single species.
Some examples are of an elongated oval form (fig. 12), such speci-
mens being nearly uniformly convex with hardly any apparent bipli-
eation in the dorsal valve, under which aspect it resembles some
examples of 7. punctata, and other closely related forms. Other
specimens have a straight or slightly indented hinge-line, with a
greater or less tendency to biplication, as in fig. 11, under which
condition they approach in shape some examples of Mr. H. E. Des-
longchamps’s 7’. dorsoplicata and even 7’. perovalis, while others,
again, are decidedly biplicated, as in figs. 13 and 14, and are not
unlike some Cretaceous specimens of 7’. biplicata and the Jurassic
T. indentata.

The same kind of variation in form, with almost similar shapes,
has been shown to occur in 7. b¢ephicata and in T. dorsoplicata, &e. ;
and, indeed, so similar and perplexing are the resemblances of the
shell under description to several congeneric forms already described,
that it is with much uncertainty that I have ventured. to apply to
the Thibet shell a distinct specific denomination.

2. RuyncHonetta Katonensts, spec. nov. Pl. I. figs. 15 &16.

Shell variable in shape, almost circular and globular, nearly as
wide as long. Valves about equally convex and deep, ornamented
with from thirteen to fourteen angular ribs, of which from three to
Six occupy a slightly elevated fold in the dorsal valve, and sinus in

38 PROCEEDINGS OF THE.GEOLOGICAL SOCIETY.

the ventral; beak incurved, of moderate projection. Proportions
variable. About 13 lines in length and breath, by 10 in depth.

Of this shell two varieties appear to occur at Kato, which may
be distinguished by the number and projection of their ribs.

§ 3. Creracrous (?) SPECIES.

A compact light grey limestone near Lacholung La, north side,
in the Suru Country in Thibet, contains in abundance two species
of Brachiopoda. The exact age of this rock does not appear to have
been hitherto satisfactorily determined ; but as these two Brachio-
pods have a very Cretaceous aspect, and as Capt. Godwin-Austen
informs me that a rock at a place called Kalatys in the Upper Indus,
not above fifty miles from where the Jurassic fossils were found,
contains Hippurites, it may not perhaps be impossible that the light
compact limestone in question may belong to the Cretaceous period.
This point, however, cannot well be determined from the examina-
tion of the two species of Brachiopoda therein found, as some- _
what similarly shaped shells do also occur in rocks of the Jurassic
period.

1. Watpurmi1a Branrorpr, spec. nov. Pl. I. fig. 8.

Shell obscurely pentagonal, straight or slightly indented in front.
Valves gently convex and smooth, no mesial fold in the dorsal
valve, but a gentle depression or sinus occurs near the front of the
ventral ; beak small, truncated by a foraminal aperture. Length
Con width 8, depth 4 lines. |

2. RuyncHonetta, sp. Pl. I. figs. 9 & 10.

Shell transversely oval, wider than long. Valves equally deep
and convex ; when well-shaped there exists in the dorsal valve a wide
very slightly elevated mesial fold, a sinus being present in the opposite
one. ‘The surface of each of the valves is ornamented with about
twenty-four angular ribs, of which five or eight occupy the fold and
sinus. These last are, however, very often shifted more to the one
or to the other side, giving the shell an unsymmetrical appearance.
Beak angular; foramen small, contiguous to the umbone. Propor-
tions variable. Length 10, width 12, depth 5 lines.

This irregularity in the position of the fold and sinus may be
occasionally noticed in many species of the genus Lthynchonella, but
is particularly prevalent in certain Jurassic forms, such as £. 7n-
constans, FR. sulcata, R. dimidiata, &c. ; mdeed so closely do some
of the specimens under description approximate in shape to some
specimens of Parkinson’s 2. sulcata, and to another species to which
Sowerby had given the name of R. dimidiata, that I would not ven-
ture for the present to indentify the Thibet fossil by any definite
specific denomination.

DAVIDSON—KASHMERE BRACHIOPODA. 39

EXPLANATION OF PLATE I.
Illustrative of Carboniferous, Jurassic, and Cretaceous (?) Brachiopoda
from Thibet.
(The figures are all of the natural size.)

CARBONIFEROUS SPECIES, FROM SHIGAR, NEAR SKARDO.
Fig. 1. Terebratula Austeniana, spec. nov.
2&3. Rhynchonella pleurodon, var. Davreuxiana, De Koninck.
4, Spirifer, sp.
3. Orthis, sp.
6. Productus semireticulatus, Martin.
r€ Hardrensis, var. Thibetensis.

Cretaceous (?) SprciEs, FRoM NEAR Lacno.una La, In THE Surv.
8. Waldheimia Blanfordi, spec. nov.
9&10. Rhynchonella, sp.
Jurassic Spectres, FROM Kato, LADAK, IN THE Surv.

11-14. Terebratula Thibetensis, spec. nov.
15 & 16. Rhynchonella Katonensis, spec. nov.

Notes on the Carzontrerous Bracutopropa collected by Caprain
Gopwin-Avsten in the Vattny or Kasumern. By T. Davunson,
Esq., F.R.S., F.G.8., &c.

(Puate IT.)

In 1864 I was requested by Mr. Godwin-Austen to examine a
series of Carboniferons Brachiopoda which his son had obtained from
limestone and shales near Shigar and Skardo, in Thibet (see p. 35), and
which I found to consist of the following species :—

4. Orthis, sp. (approaching in form to

O. Micheleni).
5. Productus semireticulatus.
6. Chonetes Hardrensis, var.

1. Terebratula Austeniana, 2. sp.

2. Spirifer? Not sufficiently complete
to be satisfactorily determined.

3. Rhynchonella pleurodon, var. Da-
vreuxiana.

The species were few in number, but bear great resemblance to
those found in rocks of a similar age in Europe and America, and
there is every reason to believe that when the Carboniferous series
of Thibet shall have been further searched that a larger number
of species will be discovered.

This year I have again had under examination a much larger
series of Brachiopoda which Captain Godwin-Austen had procured
from the Carboniferous limestone and shales which form the hills
around Vihi, in the Valley of Kashmere. The Brachiopoda abound
in a bed of limestone near the entrance of the ravine above the village
of Khoonmoo; but the lowest portion, or Zéwan bed, is stated by
Captain Godwin-Austen to contain the larger number of Brachiopoda ;
and a higher stage, still near the base of the formation, is said to
contain abundant remains of Productus. Barus may likewise be named
as one of the most fossiliferous localities. These Brachiopoda are,
however, but rarely in a good state of preservation, and most of the spe-

40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

cimens occur only in the condition of more or less mutilated and worn
fragments. Here again we find many of our common and widely
spread European and American species, along with a few that had
not yet been noticed from other parts of the world, and which indi-
cate that the Carboniferous rocks of Thibet, Kashmere, and the
Punjab belong to one great formation.

1. TeREBRATULA sAccuLus, Martin, sp.? PI. II. fig 1.
Anomites sacculus, Martin, Petref. Derb., tab. xlvi. fig. 1

Two ventral valves of a shell having much the appearance of some of
our British examples of 7’. sacculus occur in a grey-coloured limestone
from Barus.

2, AvHynis suptitita, Hall, var. PI. II. fig. 2.

Terebratula subtilita, Hall, in Howard Stansbury’s Exploration of
the Valley of the Great Salt Lake of Utah, p. 409, pl. 2. figs.
S22.

This appears to be a common prec in a grey limestone at ious
but has also been found at Barus, and is very abundant in the Punjab.

3. SPIRIFERA Ragau, Salter. PI. II. fig. 3.

Spirifera Rajah, Salter, Paleontology of Niti in the Northern
Himalaya, pp. 59 & 111. Calcutta, 1865.

Shell marginally longitudinally oval; hinge-line slightly shorter
than the greater width of the shell. _ Ventral valve convex, with a
narrow sinus or groove extending from the extremity of the beak to the
front, and along the centre of which there exists a narrow thread-like
rib. The surface of this valve is ornamented with from sixteen to
twenty rounded ribs, of which the two central ones are the largest
as well as the most prominent, each rib being again furrowed by
three, four, or five smaller ones, while the whole surface is also finely
longitudinally striated. Beak prominent and incurved ; area of mode-
rate width and divided in the middle by a triangular fissure. Dor-
sal valve convex, but less deep than the ventral. The mesial fold
is well defined and composed of a single rib at its origin, and
continues so to some distance, when a smaller lateral rib is produced
on either side, and extends to the front; the remaining portion
of the valve is covered with a similar succession of smaller rounded
ribs, simple at their origin, but soon producing a small one on each
of its lateral portions, the whole surface being also marked with fine
longitudinal strie, as well as by numerous fine concentric lines of
growth. The largest specimen I have seen, if complete, would mea-
sure in length 23, in width 22 lines.

Of this beautifully sculptured Spirifer a great many imperfect speci-
mens were found by Captain Godwin-Austen at Barus, in beds of the
Carboniferous age. At p. 59 of Colonel R. Strachey’s ‘ Paleontology
of Niti,’ this species is described and figured by Mr. Salter, who ob-
serves that ‘‘ the peculiar square shape, not very convex valves, acute
ribs, are all characters in which Spirifera Aajah approaches very near

mit
el

fr

Are

as

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Soc Vol, XXUeTT

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J |
: |
— 7
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= a
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DAVIDSON—-KASHMERE BRACHIOPODA. Al

the Spirifera Keilhavi. But the fasciculate secondary ribs are_
stronger, while the cost themselves are less deep.” At page 59 of
the work above named this shell is stated to have been derived “‘ from
the Trias beds of Spiti Pass”; but at page 111 of the same work
Mr. H. F. Blanford observes that the Spirifera Rajah (of Salter)
does not occur in the same bed with Triassic Ammonites, but in beds
decidedly below them—beds which other evidence combines to show
must be referred to the same general relative age (in the sense of
homotaxis) as the Carboniferous of Europe. This last view would be
confirmed by Captain Godwin-Austen’s observations in Kashmere,
where the species is Carboniferous.

4, Spremrrra Vrurana, spec. nov. Pl. II. fig. 4.

Shell longitudinally oval, longer than wide; hinge-line rather
shorter than the greatest width of the shell. Both valves are convex,
the ventral being the deeper; and each is ornamented with from
eighteen to twenty simple ribs. In the dorsal valve the mesial fold
is divided by a longitudinal groove, while in the middle of the sinus
of the ventral there exists a small median rib. Beak incurved ;
area of moderate dimensions. One specimen measured 15 lines in
width by about 14 in length. .

Three valves of this Spirifer were found embedded in a single spe-
cimen of limestone from Barus, in the Valley of Kashmere. It is
distinguishable from S. pinguis by its constant well-marked median
rib in the sinus of the ventral valve.

5. SprrirERA KAsHMERIENSIS, spec. nov. Pl. II. fig. 5.

Shell transversely fusiform; hinge-line long and straight, the
lateral margins becoming gradually attenuated. Ventral valve orna-
mented with about twenty simple ribs; the sinus deep and divided
along the middle by a small median slightly projecting rib, which,
commencing at a short distance from the beak, extends to the front.
Length 7, width 18 lines.

Of this Spirifer I have seen two or three ventral valves only, one of
them occurred in the same block of limestone along with S. Vihiana
obtained from the neighbourhood of Barus, the other specimens were
labelled Khoonmoo. It may be distinguished from the preceding
species by its very transverse spindle shape, and it is not very unlike
in form some examples of S. macropterus, Goldf., but may be distin-
guished by the presence of the small median rib in the sinus.

6. Sprrrrera Moosaxwarensis, Dav. PI. II. fig. 6.

Spirifera Moosakhailensis, Dav. Quart. Journ. Geol. Soc. vol. xviii.
p- 28, pl. 2. fig. 2.

Two or three specimens, agreeing in character with those I have
already described from the Carboniferous limestone of Moosakhail and
Kafir Kote, in the Punjab, were found at Barus. Prof. E. Beyrich
informs us also that this shell was found in the Carboniferous lime-
stone of the Island of Timor.

42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

7. SPIRIFERA BARUSIENSIS, spec. nov, UPI. Dipfie: ‘7%

Shell subr homboidal; hinge-line straight and as long as the width
of the shell ; cardinal oxtr emities angular and proj jecting ; ; Sinus wide.
Surface ornamented with about fineen ribs, those in the sinus being
much smaller than those on the lateral portions of the valve. Length
24, width 5 lines.

Of this small Spirifer a single ventral valve was found in the
Carboniferous shales or Zéwan beds of the Valley of Kashmere. It is
quite different in shape and character from the other three species, and
remarkable on account. of the great comparative width of its sinus.
The description of this shell and that of S. Kashmeriensis are neces-
sarily very incomplete, since our material consists of ventral valves
only.

8. Ruyncnonrttsa Barumensis, spec. nov. Pl. II. fig. 8.

Shell elongated, subtrigonal; dorsal valve convex, the mesial fold
being very wide and composed of three ribs, of which the central
is the most elevated; three smaller ribs occupy each of the lateral
portions of the valve. Ventral valve rather deeper than the opposite
one, the wide sinus having two ribs, while three or four smaller ones
occupy each of the lateral portions of the valve. Beak much pro-
duced and incurved at its angular extremity. The lateral portions
of the ventral valve at and ncar the beak are much depressed and
form a convex curve, which indents to a considerable extent the
corresponding portion of the dorsal.

Of this species two longitudinal halves only were found m the
Zéwan beds, Valley of Kashmere ; but they were sufficiently perfect
to enable me to accurately restore the wanting portions. ‘The largest
example measured, when perfect, 9 lines in leneth, by 7 in width, ‘and
4in depth. It bears a certain resemblance to some examples of Rhyn-
chonella angulata, Linn., with which, however, it cannot with cer-
tainty be identified.

9. RHYNCHONELLA KAsMERIENSIS, spec. nov. PI. II. fig. 9.

Shell oblato-deltoidal, wider than long. Ventral valve convex,
with a wide deep sinus possessing four or five rounded ribs of unequal
width, namely, a small central one intervening between two larger
ones. Three or four ribs occupy also each of the lateral portions of
the valve. Beak small, incurved. Dorsal valve convex, smooth at the
umbone; mesial fold wide, evenly convex, and ornamented with four
ribs, three others occupying each of the lateral portions of the valve
in the contiguity of the margin.

Of this shell a single specimen was found in the Zéwan beds, Valley
of Kashmere; in form it approaches some examples of R. pugnus,
but differs by the shape of the ribs in the sinus. The study of more
specimens would be desirable.

10. SrrEPTORHYNCHUS CRENISTRIA, Phillips. Pl. II. fig. 10.

Spirifera crenistria, Phillips, Geol. of owas vol,’ 1) pltise
fie, |G.

DAVIDSON—-KASHMERE BRACHIOPODA. 43

Several examples agreeing with those found in Europe have been
obtained at Barus and in the Zéwan beds, in the valley of Kashmere.
The species occurs also in the Punjab.

11. Srreproruyncuus, ? sp. PI. II. fig. 11.

‘One imperfect valve appears referable to another species of this
subgenus, but the specimen was not. sufficiently complete to admit of
its specific distinctions or characters being satisfactorily determined.
The valveis about 5 linesin length by 7 in width, moderately convex,
and ornamented with about eight rounded ribs, three or four smaller
longitudinal ones occupying the wide interspace left between thelarger.
From the Zéwan beds, in the Valley of Kashmere.

12. Propucrus SEMIRETICULATUS, Martin, sp. Pl. II. fig. 12.

Anomites semircticulatus, Martin, Petrif. Derb. pl. xxxili. figs.1 & 2,
and pl. xxxiil. fig. 4.

A large variety of this well-known and far spread species is
exceedingly abundant at Barus, and is indeed (along with Spirifera
Austenana and .Athyris subtilita) the Brachiopod most commonly
found, but unfortunately apparently always in avery bad or indifferent
state of preservation; it occurs also near Loodco west of Wasterwan
A smaller variety has been found in the Punjab and also in Thibet.

13. Propvcrus cora, D’Orbigny.
Productus cora, D’Orbigny, Paléontologie du Voyage dans I’ Amé-
rique Méridionale, pl. v. figs. 8, 9, & 10.
Three or four specimens referable to this species have been found
at Barus; it occurs also in the Punjab, and is very common in
Europe.

14, Propuctrvs scapricvius, Martin. Pl. IT. fig. 13
Anomates scabriculus, Martin, Petrif. Derb. p. 8, pl. xxxi. fig. 5.
Of this well-known species some examples were found at Barus
and Khoonmoo. :
15. Propvctus Humnotpti, D’Orb. PI. II. fig. 14.

Productus Humboldiw, D’Orb. Paléont. du Voy. dans l’ Amérique
Meéridionale, pl. 5, fies. 4—7,

Two fragments referable to this species were found at Khoonmoo,

and in the Zéwan beds, Valley of Kashmere ; it is also common in
the Punjab.

16. Propvucrus tonerspmnvs, Sow. ?
Productus longispinus, Sow. Min. Conch. vol. i. p? 154, pl. xviii.
fie. 1,
Of this species an imperfect example was obtained from the grey

limestone at Khoonmoo. It is exactly like some specimens found in
the Punjab.

44. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

17. Propucrus striatus, Fischer ?

Mytilus striatus, Fischer, Oryct.du Gouy.de Moscow, p.181, pl. xix.
fio A
A fragment, having much the appearance of haying belonged to
this well-known species, was found at Barus, in the Valley of Kash-
mere, but the specimen was not sufficiently complete to warrant a
certain identification. The shell is not rare in the Punjab.

18. Propuctus sprnutosus?, Sow. PI. IL. fig. 15.

Two specimens, bearing much resemblance to some of our European
examples, were obtained from the grey limestone of Khoonmoo. The
shell is small, transversely semicircular ; the ventral valve regularly
convex, without sinus; surface covered with numerous subregular
small tubercles, somewhat quincuncially arranged (each tubercle
having given rise in the perfect shell to a slender spine) ; the con-
centric wrinkles are also slightly marked, and on one specimen
somewhat as we find to be the case in P. Keyserlingiana, or even P.
Deshayesiana, De Koninck, to which these Kashmere shells bear
some resemblance.

19. Propuctus Lavis, spec. nov. PI. II. fig. 16.

Shell small, nearly circular; hinge-line slightly shorter than the
greatest width of the shell; ventral valve evenly convex ; ears small;
surface smooth? Length 3 lines, the width slightly exceeding that
of the length.

Of this small species a single ventral valve has been discovered,
but it was so distinct, both by its shape and surface, from other known
species of the genus that I have ventured to apply to it a distine-
tive designation. It occurs in a coarse limestone in the Zéwan beds,
Valley of Kashmere, but less compact and of a lighter grey than the
bed from which most of the species found at Khoonmoo were
obtained.

20. Propuctus, sp. ?

A fragment of internal cast indicates the presence of another species,
but not specifically determinable from the material in our possession.
Barus.

21. CHonrres LazvIs, spec. nov. Pl. II. fig. 17.

Shell marginally semicircular, concavo-convex ; hinge-line straight,
about as wide as the width of the shell; each valve is provided with
a subparallel area, which is widest in the ventral valve; ventral
valve moderately convex, flattened towards the ears; surface smooth?
Length 4, width 6 lines. Of this Chonetes two or three more or less
complete specimens occur on a fragment of limestone from Barus, in
the Valley of Kashmere.

22. CuonnTEs? AUSTENIANA, Spec. noy. Pl. II. fig. 18.

Shell marginally transversely semicircular ; hinge-line straight, as
wide as the shell; ventral valve moderately convex, with a narrow

DAVIDSON—-KASHMERE BRACHIOPODA. 45

median concave groove commencing at the extremity of the beak and
extending to the front; four obscure rounded ribs of very small ele-
vation may be traced on the lateral portions of the valve in contiguity
as to the central groove. I have seen but a single incomplete spe-
cimen of this species, which occurs in the same coarse light-grey
limestone which contains Productus levis. From the Zéwan beds,
Valley of Kashmere.

23. Discrva KasHmeErrensts, spec. noy. PI. II. fig. 19.

Shell marginally ovate or longitudinally oval, the posterior portion
being narrower than the anterior. The imperforate valve is con-
vex, and most elevated towards the middle, the rounded apex
sometimes projecting beyond the level of the posterior margin.
Surface smooth. Length 13, width 11 lines.

Of this curious species two specimens were found at Khoonmoo, in
the Valley of Kashmere.

EXPLANATION OF PLATE II.
Iilustrative of Carboniferous Brachiopoda from Kashmere.
(The figures are all of the natural size.)

. Terebratula sacculus, Martin. Barus.

. Athyris subtilita, Hall, var. Barus and Khoonmoo.

. Spirifera Rajah, Salter (partly restored). Barus.
Vihiana, spec. nov. Barus.

. —— Kashmeriensis, spec. nov. Barus and Khoonmoo.

Fig. 1
2
3
4
5
: —— Moosakhailensis, Dav. Barus.
8
2
10

Barusiensis, spec. noy. Zéwan beds.

. Rhynchonella Barumensis, spec. nov. Zéwan beds.
Kashmeriensis, spec. nov. Zéwan beds.

. Streptorhynchus crenistria, Phillips. Barus and Zéwan beds.
, 8p. Zéwan Beds.

12. Productus semireticulatus, Martin. Barus,

scabriculus, Martin. Barus and Khoonmoo.

14. —— Humboldtti, D’Orb. Khoonmoo and Zéwan beds.
spinulosus?, Sow. Khoonmoo.

levis, spec. nov. Zéwan beds.

17. Chonetes levis, spec. nov. Barus.

? Austeniana, spec. nov. Zéwan beds.

19. Disetna Kashmeriensis, spec. noy. Khoonmoo.

46

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From July 1st to September 30th, 1865.

I. TRANSACTIONS AND JOURNALS.

Presented by the respective Societies and Editors.

Abbeville. Mémoires de la Société Impériale d’Emulation d’Abbe-
ville. Premicre Partie. 1861-65.

B. de Perthes.—Découverte d’une machoire humaine dans le dilu-
vium, l.

Milne-Hdwards—Sur les résultats fournis par une enquéte relative
a la découverte d’une machoire humaine et de haches en silex,
dans le terrain diluvien de Moulin-Quignon, 75.

B. de Perthes.—Nouvelles découvertes d’os humains dans le dilu-
vium, en 1863 et 1864, 91.

Albany Institute. Transactions. Vol. u. No.1. 1833. rom
Sir R. I. Murchison, Bart., K.C.B., F.GS., fe.

American Academy of Arts and Sciences. Vol.vi. January to June
1864.

American Association for the Advancement of Science. Proceedings
of the Second Meeting, held at Cambridge, August 1849. rom
Sir R. I, Murchison, E. C.B., LG Se.

R. W. Gibbes—Mosasaurus and other allied genera in ihe United
States, 77.

J.C. Warren.— Mastodon angustidens, 93.

J. D. Dana.—Isolation of Volcanic action in Hawaii, 95.

L. Agassiz.—Fossil Remains of an Elephant found in Vermont, 100.

L. Saemann. —Remarks on Boltonite, 105.

B. Silliman, jun.—On Boltonite of Shepard, and Bisilicate of Mises
nesia of Dr. Thomson, 109.

Identity of Sillimanite of Bowen, of Bucholzite of Brandes,

and of Fibrolite of Bournon with the species Kyanite, 111.

On “Indianite” of Count Bournon, 181.

—. Analyses of “Green Picrolite” and Slaty Serpentine,” so
called, from Texas, 154.

DONATIONS. 47

American Association for the Advancement of Science. Proceedings
of Second Mecting, 1849 (continued).

K. Hitchcock.—River Terraces of the Connecticut Valley, and on
the Erosions of the Earth’s Surface, 148.

C. Hartwell and E. Hitchcock, jun.—Description of certain Mineral
Localities in Massachusetts, 159.

H. D. Rogers.—Analogy of the Ribbon Structure of Glaciers to the
Slaty Cleavage of Rocks, 181.

R. W. Gibbes.—New Species of Fossil Myhobates from the Kocene
of South Carolina, and New Fossils from the Cretaceous, Eocene,
and Pliocene of South Carolina, Alabama, and Mississippi, 193.

Hi. D. Rogers.—Origin of the Drift, and of the Lake and River Ter-
races of the United States and Hurope, 239.

W. C. Redfield.—Fossil Remains from Broome County, 255.

C.T. Jackson.—Geology, Mineralogy, and Mines of Lake Superior, 283.

—. Geological Structure of Keweenaw Point, 288.

J. 8. Hodge.—Mineral Region of Lake Superior, 301.

A. Guyot.—Erratic Phenomena of the White Mountains, 308.

—. Erratic Phenomena of the Central Alps, 311.

J. D. Dana.—Trend of Islands and Axis of Subsidence in the Pacific,
321.

T. S. Hunt.—Geology of Canada, 325.

M. F. Maury.—Sediment of the Mississippi, 334.

J. Hall.—Brachiopoda of the Silurian Period, 347.

Graptolites, their Duration in Geological Periods, and their
Value in the Identification of Strata, 351.

Baird.—Bone-caves of Pennsylvania, 352.

L. Feuchtwanger.—Discovery of a new Cave in Kentucky, 355.

J. W. Bailey.—Process for detecting the Remains of Infusoria, &c.,
in Sedimentary Deposits, 409.

American Journal of Science. Second Series. Vol. xl. No. 118.
July 1865.

L. Lesquereux.—Origin and Formation of Prairies, 23.

F. B. Meek.—Notice of a small collection of Fossils found by Dr.

Hays on the west shore of Kennedy Channel, 31.
T. S. Hunt.—Contributions to the Chemistry of Natural Waters, 43.
C. U. Shepard.—Mineralogical Notices, 110.
J. H. McChesney.—New Species of Fossils from the Paleozoic Rocks
of the Western States, 116.
J. P. Lesley.—Mont Alto Lignite and Appalachian Erosion, 119.
Fouqué.—EHruption of Etna, 122.

Coan.—Voleano of Kilauea, 122. :
Shepard.—Additional Notes on the Minerals of the Emery-mine at
Chester, Massachusetts, 123.

Geological Map of Russia, 123.

R. N. Rubidge.—Changes rendered necessary in the Geological Map
of South Africa, 123.

R. Owen.—Anthrakerpeton, a new Carboniferous Reptile, 124.

De Morner.—Mineral Wealth of Mexico, 124.

A. Sismonda.—Gneiss with the Impression of an Equisetum, 124.

H. 8t.-C. Deville-—Kalicine, 124.

F. H. Bradley.—Geological Excursion, 125.

Messikomer.—Lake-habitations, 135.

P. J. van Beneden and EH. Dupont.—Human Remains of the Trou du
Frontal, 136,

48 DONATIONS.

Assurance Magazine. Vol. xii. Part 4. July 1865.

Atheneum Journal. Nos. 1966-1979. July to September 1865.

Notices of Meetings of Scientific Societies, &c.

J. J. Lake.—Geology of the Mediterranean, 26.

G. Greenwood.— Lyell on the Weald ; Drew on Romney Marsh,” 184.

Discovery by the Rey. W. Fox of a new Saurian in the Weald near
Brooke, Isle of Wight, 186.

A. Geikie’s ‘The Scenery of Scotland viewed in connexion with its
Physical Geography,’ noticed, 207.

R. G. M. Browne’s ‘ Astronomical Geology: a treatise respecting the

~ Causes to which the structural and superficial Configuration of the
Earth’s Crust is attributed,’ noticed, 250. —

Mineral Statistics of the United Kingdom for 1864, 251.

H. Lecoq’s ‘Mineral Waters regarded in relation to Chemistry and
Geology,’ noticed, 281.

Meeting of the British Association, 338, 372, 403, 438.

The Stone Age, 402.

Berlin. Zeitschrift der deutschen geologischen Gesellschaft. Vol. vil.
Heft 1. November and December 1864, and January 1865.

C. Rammelsberg.—A. Scacchi, tiber die Polysymmetrie der Krystalle,
30 (plate).

Bemerkungen zu Scacchi’s Abhandlung ther die Polysym-
metrie und zu der von Des Cloizeaux tiber die Pseudodimorphie, 56.

G. Tschermak.—Bemerkungen zu dem Aufsatze des Herrn G. Rose:
‘Ueber die in den Thonschiefern vorkommenden, mit Faserquarz
bedeckten Hisenkieshexaéder, 68.

H. von Dechen.—Vergleichende Uebersicht der vulkanischen Erschei-
nungen im Laacher See-Gebiete und in der Eifel, 69.

H. Credner.—Die Zone der Opis similis, Phill. im Oxford, yon Han-
nover, 157 (plate).

. Geognostische Beschreibung des Bergwerksdistrictes von St.
Andreasberg, 163 (8 plates).

——. Die Verbreitung des Gault in der Umgegend von Hannover,
232 (plate).

Boston. American Journal of Conchology. Vol.i. No.3. July 1865.,

Boston Society of Natural History. Proceedings. Vol. vil. pp. 145-
448. November 1859 to February 1861.

C. T. Jackson.—Crystals of Green Felspar from the Sea-wall near
Southwest Harbour, Mount Desert, Maine, 160.

W. B. Rogers.—Fossil Cast in Sandstone of part of the Trunk of a
large Sigillaria from South Joggins, Nova Scotia, 168. :

E. Hitchcock, jun.—On the elongated, flattened, and curved pebbles

_ found in the Conglomerate of Vermont, 208.

C. H. Hitchcock.—Explanation of a Geological Map of Vermont, 236.

W. B. Rogers.—Stratigraphical Relations of Marine Deposits, 246.

R. Field.—Footmarks of the Connecticut River Sandstones, 316.

©. A. White.—Geology and Paleontology of Burlington, lowa, and
its Vicinity, 319.

E. Hitchcock.—Conglomerate of Vermont, 358.

J. Marcou.—Primordial Fauna, and Taconic System, 369.

N. Easton.—Imprints of Shells in Siliceous Slate of Fall River, 389.

W. B. Rogers.—Remarks on the Group of Rocks constituting the
base of the Palaeozoic Series in the United States, 394.

DONATIONS. 49

Boston Society of Natural History. Proceedings. Vol. vii. pp. 145-
~ 448 (continued).
W. B. Rogers.—Palseozoic Rocks of Dennis River in Maine, 419.
CO. H. Hitchcock.—Geology of Vermont in relation to the Taconic
System, 426.

Vol. ix. pp. 321-886. February and March 1865.

Breslau. Abhandlungen der Schlesischen Gesellschaft fur vaterlan-
dische Cultur. Abtheilung fiir Naturwissenschaften und Medicin.
1864. Heft 1.

. Philosophisch-historische Abtheilung. Heft 2. 1864.

Zwei und vierzigster Jahres-Bericht der Schlesischen Gesell-
schaft fiir vaterlindische Cultur. 1864.

Websky.—Ueber die Bestrebungen franzdsischer Mineralogen, die
Erscheinungen, welche die durchsichtigen Mineralkorper im polari-
sirten Lichte darbieten, als wesentlich bestimmendes Kennzeichen
in Anwendung zu bringen, 23.

Runge.—Ueber die nunmehr vollstindig publicirte geognostische
Karte des niederschlesischen Gebirges, 24.

F, Rémer.—Die Kattowitzer marine Conchylien-Fauna auch bei
Rosdzin entdeckt, 25.

Ueber ein kreisrundes, scheibenformiges Gneisgeschiebe aus

dem Karolinen-Flotze bei Kattowitz, 26.

Ueber die Auffindung eines fossilen Saugethiers in der Tertiar-
bildung von Dirschel, 27.

—. Ueber eine in den Monaten Marz und April d. J. gemachte
Reise nach Spanien, 27.

‘Erlauterung des Berichts tiber die Erhebungen der Wasser-

Versorgungs-Commission des Gemeinderathes der Stadt Wien ;

Wien 1864’ noticed, 30.

Ueber ein Vorkommen von Cardiwm edule and Buccmum reti-

culatum in dem Diluvial-Kies bei Bromberg, 32.

Ueber ein Stiick des am 14. Mai 1864 bei Orgueil gefallenen
Meteoriten, 32.

F. Cohn.—Ueber die Entstehung des Travertin in den Wasserf illen
von Tivoli durch Vermittelung der Moose und Algen, 32.

Goppert.—Ueber die Darwin’sche Transmutations-Lehre mit Bezie-
hung auf fossile Pilanzen, 39.

——ee
e

British Association for the Advancement of Science, Report of the
Thirty-fourth Meeting, held at Bath in September 1864. 1865.

P. de M. G. Egerton, T. H. Huxley, and W. Molyneux.—Distribution
of the Organic Remains of the North Staffordshire Coal-field, 342.
Daubeny.—Thermal Waters of Bath, 26.
Roscoe.—Existence of Lithium, Strontium, and Copper in the Bath
Waters, 41.
W. L. Scott.—New Sources of Thallium, 41.
J. Phillips—Address to Geological Section, 45.
W. H. Baily.—New points in the Structure of Palechinus, 49.
Occurrence of Fish-remains in the Old Red Sandstone at
Portishead, near Bristol, 49. '
H. B. Brady.—Foraminifera of the Middle and Upper Lias of Somer-
setshire, 50.
H. W. Bristow.—Rheetic (or Penarth) Beds of the Neighbourhood of
Bristol and the South-west of England, 50.
VOL. XXII,—PART I. B

50 DONATIONS.

British Association for the Advancement of Science. Report, 1864
(continued).

P. B. Brodie.—Two outliers of Lias in South Warwickshire, and pre-
sence of the Rhetic Bone-bed at Knowle, 52.

P. P. Carpenter.—Connexion between the Crag Formations and the
recent North Pacific Faunas, 52.

Daubeny.—Cause of the Extrication of Carbonic Acid from the In-
terior of the Earth, and on its Chemical Action upon the Consti-
tuents of Felspathic Rocks, 52.

W. B. Dawkins.—Newer Pliocene Fauna of the Caverns and River-
deposits of Somersetshire, 53.

R. Harkness.—Lower Silurian Rocks of the South-east of Cumber-
land and the North-east of Westmoreland, 53.

J. Hector.—Geology of the Province of Otago, New Zealand, 54.

Hennessy.—Possible Conditions of Geological Climate, 55.

W. Keene.—Coal-measures of New South Wales with Spircfer,
Glossopteris, and Lepidodendron, 58.

E. R. Lankester.—Species of the genus Péeraspis, 58.

J. Leckenby.—Boulder-clay and Drift of Scarborough and Hast
Yorkshire, 58.

C. Moore.—Geology of the South-west of England, 59.

C. W. Peach.—Traces of Glacial Drift in the Shetland Islands, 59.

ars Additional List of Fossils from the Boulder-clay of Caithness,

W. Pengelly.—Accumulation of Shells, with Human Industrial
Remains, found on a hill near the River Teign, in Devonshire, 65.

Changes of Relative Level of Land and Sea in South-eastern
Devonshire in connexion with the Antiquity of Mankind, 63.

J. Phillips.—Formation of Valleys near Kirkby Lonsdale, 63.

——. Measure of Geological Time by Natural Chronometers, 64.

——. Distribution of Granite Blocks from Wasdale Craig, 65.

W. B. Rogers.—Peculiar Fossil found in the Mesozoic Sandstone of
the Connecticut Valley, 66.

R. N. Rubidge.—Relations of the Silurian Schist with the Quartzose
Rocks of South Africa, 66.

J. W. Salter.—New Forms of Olenoid Trilobites from the Lowest
Fossiliferous Rocks of Wales, 67.

. Old Pre-Cambrian (Laurentian) Island of St. David’s, Pem-
brokeshire, 67.

W. Sanders.—Explanation of a Geological Map of the Bristol Coal-
field, 68. |

W. A. Sanford.—Carnassial and Canine Teeth from the Mendip
Caverns, probably belonging to Felis antiqua (syn. Pardus), 69.

H. Seeley.—Significance of the Sequence of Rocks and Fossils, 69.

W. W. Smyth.—Thermal Water of the Clifford Amalgamated Mines
of Cornwall, 70.

H. C. Sorby.—Conclusion to be drawn from the Physical Structure
of some Meteorites, 70.

W. W. Stoddart.— Lowest Beds of the Clifton Carboniferous Series, 71.

H. B. Tristram.—Bone Breccia with Flints in Lebanon, 72.

. Sulphur- and Bitumen-deposit at the South-west Corner of
the Dead Sea, 73.

H. Woodward.—Family of the~ Ewrypterida, with descriptions of
some new genera and species, 73.

T. Wright.—Development of Ammonites, 73.

——. White Lias of Dorsetshire, 75.

DONATIONS. 5L

Brussels. Annuaire de Académie Royale des Sciences, des Lettres,
et des Beaux-Arts de Belgique. 31° Année. 1865.

—. Bulletins de Académie Royale des Sciences, &e., de Belgi-.
que. 33° Année, 2°Sér. Vol. xviu. 1864.

D’Omalius.—Sur les échantillons de phosphate de chaux découverts
a Ramelot par M. Dor, 547. i

Dewalque.—Note sur le gisement de la chaux phosphatée en Belgi-

ue, 8.

Be Kaninck, A. de Vaux, et Dewalque.—Sur l’eau minérale du puits
artésien d’Ostende, 113, 119, 121.

Malaise.—Note sur le terrain crétacé de Lonzé, 317.

D’Omalius.—Rapport sur un mémoire de M. E. Dupont concernant
les assises du calcaire carbonifére des environs de Dinant, 311.

H. Nyst.—Notice sur une nouvelle espéce de Pecten et observations
sur le Pecten Duwelsir, 26.

EK. Dupont.—Sur les fouilles faites dans le Trou des Nutons, prés de
Furfooz, 30, 228, 387.

Coemans et Kickx, jun.—Monographie des Sphenophyllum d’Kurope,
134.

Van Beneden.—Découverte d’une pince de homard dans une pierre
de V’argile de Rupelmonde, 133.

Malaise.—N ote sur l’existence en Belgique de nouveaux gites fossili-
féres 4 faune silurienne, 321.

Dewalque.—Une nouvelle dent de Carcharodon dans le gravier de la
Meuse, 400.

ievAvmce Oetér Vol xixe 1865,

Van Beneden et E. Dupont.—Sur les ossements humains du Trou du
Frontal, 15.

Nyst.—Sur une coquille fossile du systéme Diestien, nouvelle pour la
faune belge, appartenant au genre Modiola, 30.

_—

Mémoires couronnés et mémoires des savants étrangers,
publiés par l’Académie Royale des Sciences, &c., de Belgique.
Vol. xxxii. 1864-65.

Mémoires couronnés et autres mémoires publiés par |’ Aca-
démie Royale des Sciences, &c., de Belgique. Vol. xvii. 1865.

A. Perrey.—Note sur les tremblements de terre en 1863, avec supplé-
ments pour les années antérieures, de 1848 4 1862.

Calcutta. Journal of the Asiatic Society of Bengal. Part I. No.1,
and Part II. No.1. 1865.
A. M. Verchere.—Notes to accompany a Geological Map and Section

of the Lower Ghur, or Sheen Ghur range, in the district of Bun-
noo, Punjab, with analyses of the Lignites, 42 (plate).

Canadian J ournal. New Series. Vol. x. Nos. 57 &58. May to
July 1865.

Canadian Naturalist and Geologist. New Series. Vol. ii. No. 3.
June 1865.

T. Sterry Hunt.—Contributions to the Chemistry of Natural Waters,
II. Analyses of Various Natural Waters, 161.

E 2

52

DONATIONS.

Canadian Naturalist and Geologist. New Series. Vol. ii. No. 3

(continued).

E. Billings.—On some of the more remarkable genera of Silurian and
Devonian Fossils, 184.

H. F. Perley.—Gold-mines ana Gold-mining in Nova Scotia, 198.

T. Macfarlane.—Extraction of Copper from its Ores, 219.

D. W. Bailey, G. F. Matthew, and C. F. Hartt’s s ‘Geology of New
Brunswick,’ noticed, 232.

Ye indica: Report on the Geology of New Brunswick,’ noticed,
232.

Chemical Society. Journal. Second Series. Vol.ii. Nos. 29-31.

May to July 1865.

Colliery Guardian. Vol. x. Nos. 235-248. July to September

1865.

Belgian Bone-caves, 10.

Manchester Geological Society, 10.

Dudley Geological Society, 23, 142.

Discovery of Cannel Coal in New South Wales, 51.

North of England Institute of Mining Engineers, 39, 48, 65.
Coal in New Zealand, 51.

Mineral-field of Southern Ohio, 51, 75, 90.

Discovery of Fossil Shells in the Silurian Rocks of Moffat, 74.
Geological Discoveries at Harrington, 103.

Lower Coal-measures of Monmouthshire, 122.
Gold-mining in Wales, 123.

Mineral Statistics of the United Kingdom, 124.

Petroleum in West Virginia, 136.

Meeting of British Association, 189, 192, 212, 215, 2381, 233.
Discovery of Fossil Trees at Tronbridge; 249,

J. Skidmore, jun.—The Stourbridge Vire-clay, 252.

Dijon. Mémoires de l’Académie Impériale des Sciences, Arts, et

Belles-Lettres. 10° Série.. Vol. x. 1862. #Hrom Sir R. I.
Murchison, Bart., K.C.B., F.GS., &e.

J. Martin.—Note sur quelques fossiles nouveaux ou peu connus de
Vétage bathonien de la Cote-d’Or, 55 (5 plates).
J. le Conte.—Sur les Plantes des Terrains Carboniféres, 105.

Geological Magazine. Vol. u. Nos. 13-15. July to September

1865.

Geological Progress. No. I., 289.

J. Phillips. —Oxford Fossils. No. I., 292 (plate).

R. D. Darbishire-—Genuineness of certain Fossils from the Maccles-
field Drift-beds, 293.

D. Mackintosh.—Tourist’s Notes on the Surface-g geology of the Lake-
district, 299.

T. R. Jones.—Microzoa of the Valley-deposits of the Nar, Norfolk,
306.

A. L. A. Fée’s ‘Le Darwinisme: ou, Examen de la Théorie relative
i VOrigine des Espéces,’ noticed, 308,

Memoirs of the Geological Survey ‘of India, Vol. iii. Part 2, noticed,
310.

H. B. Holl’s ‘Formation and History of the Malvern Hills,’ noticed,
316,

DONATIONS. 53

Geological Magazine. Vol. ii. Nos. 13-15 (continued).

Geological Progress. No. I. Field-clubs and Local Geological So-
cieties, 337.

R. Owen.—New Genus (Miolophus) of Mammal from the London
Clay, 339 (plate).

C. W. Peach.—Traces of Glacial Drift in the Shetland Islands, 341.

D. C. Davies.— Walk over the “ Ash-bed” and “ Bala Limestones”’
near Oswestry, 343.

Daglish and Forster.—Maenesian Limestone of Durham, 355.

C.V ogt’s ‘Lectures on Man; his Place in Creation and in the Her
of the Karth,’ edited by De. J. Hunt, noticed, 357.

W. H. Baily. —Cambrian Rocks of the British Islands, with especial
reference to the occurrence of this Formation and its Fossils in
Ireland, 385.

Extinct Gigantic Armadillo, 400.

H. Woodward.—Crustacean Teeth from the Carboniferous and Upper
Ludlow Rocks of Scotland, 401 (plate).

E. W. Binney.—Remaris on ‘the genus Polyporites, 404.

R. Owen.—Observations on ‘Recherches sur les Squalodons’ by P.
J. Van Beneden, 405.

J. Hall’s ‘Graptolites of the Quebec Group,’ noticed, 413.

J. F. Campbell’s ‘ Frost and Fire, Natural Engines, Tool-marks and
Chips, with Sketches taken at home and abroad,’ noticed, 415.

‘Short American Tramp in the Fall of 1864,’ noticed, 415.

T. Marsden’s ‘Sacred Steps of Creation; or, the Revealed Genetic
Theology illustrated by Geology and Astronomy,’ noticed, 417.

Abstracts of British and Foreign Memoirs, 307, 347; 405.

Reports and Proceedings of Societies, 318, 362, 420.

Correspondence, 326, 377, 428.

Miscellaneous, 330, 383, 432,

Geological and Natural History Repertory. Vol.i. No.4. 1865.

J. Jones.—Trees of the Stone, Bronze, and Iron Ages, 73.
S. J. Mackie.—Undescribed Vegetable Fossil, 79.
Correspondence, 71, 80.

Proceedings of Societies, 82.

Bibliographical Notices, 82.

Geologists’ Association. Proceedings. Vol.i. No.11. 1864-65,

W. Hislop.—Notes on Microscopic Geology, 373, 378, 386.

C. Evans.—Excursion to Sevenoaks, 390.

C. B. Rose.—Recent Marine Deposit at Boulogne, 402.

A. Ramsay, jun.—Excursion to Bromley, 404.

R. ee Guppy.—Metamorphism in certain Strata at Bendigo, Australia,
09.

(.-Tomlinson.—Two Days at the Chesil Bank, 414.
T. B. Redwood.—Metal Magnesium, 415.

Intellectual Observer. Vol. vii. Nos. 42-44. July to September
1865.
Notices of Meetings of Scientific Societies, &c.
Campbell’s ‘ Frost and Hire, Natural Engines, Toolmarks and Chips,’

noticed, 9.
HL. Woodward,—Excursion to the Crag District, 35 (plate).

54 DONATIONS.

Linnean Society. Transactions. Vol. xxv. Part 1. 1865.

Liverpool Geological Society. Proceedings. 1864-65.

G. H. Morton.—Report on the Field-meeting at Llangollen, 3.

——. Report on the Field-meeting at Bidston Hill, 4.

Records of Geological Time, 5.

C. R. Hall—Conjectural Hints towards determining the Ancient
Coast-line of North Wales, between the River Dee and the Island
of Anglesea, 7 (plate).

Ki. A. Eskrigee.—Geology of the Country around Builth, 20.

G. H. Morton.—Recent Shell-bed at Wallasey, 26.

H. F. Hall.—Geological Ramble in Ireland, 27.

D. C. Davies.—List of Fossils from the Bala Limestone and its asso-
ciated beds in North Wales, 30.

T. J. Moore.—Footprint of Iguanodon, 35.

H. Duckworth.—Description of part of the lower jaw of a large
Mammal, probably of Deinotherian type, from Perim Island, 38.

Historic Society of Lancashire and Cheshire. New Series.
Vol. iv. Session 1863-64.

London, Edinburgh, and Dublin Philosophical Magazine. Vol. xxx.
Nos. 200-202. July to September 1865. From Dr. W. Francis,

D. Forbes.—Researches on the Mineralogy of South America, 139.

G. F. Matthew.—Azoic and Paleozoic Rocks of Southern New
Brunswick, 15.

F. Sandberger.—Results of Geological Observations in Baden and
Franconia, 158.

R. N. Rubidge.—Changes rendered necessary in the Geological Map
of South Africa, 159.

London Review. Vol.x. Nos. 261-274. July to September 1865.

Notices of Meetings of Scientific Societies, &c.

J. Kelly’s ‘Notes on Errors in Geology,’ noticed, 46.
Ancient Rhone Glacier, 253.

S. Haughton’s ‘ Manual of Geology,’ noticed, 261.
Meeting of the British Association, 275, 307, 351.

Longman’s Notes on Books. Vol. iti. No. 42. August 31, 1865.
S. Haughton’s ‘ Manual of Geology,’ noticed, 26.

Lyon. Bulletin des Séances de l’Académie Impériale des Sciences,
Belles-Lettres, et Arts. January to March 1865. »

Milan. Atti della Societ&é Italiana di Scienze Naturali. Vol. vi.
Fase. 4 & 5. October 1864 and March 1865.

Meneghini.—Studj paleontologici sulle ostriche cretacee della Sicilia,
410 (plate).

Pecchioli.—Descrizione di alcuni nuovi fossili delle argille subapen-
nine toscane, 498 (plate).

De Mortillet.—Géologie des environs de Rome, 530.

Bellii—Sulle maree delle rocce liquide sotto la crosta terrestre, 539..

Zollikofer.—Esposizione dei differenti sistemi geologici, 545. i

DONATIONS. 55

Milan. Atti della Societé Italiana di Scienze Naturali. Vol. vii.
1864.
Issel.—Di una caverna ossifera di Finale, 175 (plate).
Haidinger.—Recenti lavori dell’ Istituto geologico di Vienna, 203.
Balsamo-Crivelli.—Di una vertebre fossile di rettile, 210.
Stoppani.—Risultati geologici dedotti dallo studio delle grandi bivalve
cardiformi, 213 (plate).

——. ——. Vol. viii. Fasc.1. April 1865.

Indicazioni relative alla Commissione di geologia nel Portogallo, 65

Omboni.—Relazione sulle condizioni geologiche delle ferrovie pro-
gettate per arrivare a Coira passando per lo Spluga, il Settimo, e il
Lucomagno, 96.

Munich. Sitzungsberichte der kénigl.-bayer. Akademie der Wissen-
schaften. Vol.i. Hefte 3&4. 1865.

New York. Annals of the Lyceum of Natural History. Vol. viii.
Nos. 2&3. June to December 1864.

Charter, Constitution, and By-laws of the Lyceum of Natural
History, with a List of the Members, &. 1864.

Palermo. Giornale di Scienze Naturali ed Economiche. Vol. i.
Fase. 1. 1865.

G. G. Gemmellaro.—Nerinee della ciaca dei dintorni di Palermo, 6
(4 plates).

Paris. Annales des Mines. Sixieme Série. Vol. vii. Livr. 2 & 3.
1865.
Bee Nuc sur les sources minérales de la province d’Alger,
157.

——. Analyses de diverses eaux minérales de la province d’Alger,
233.

Bulletin de la Société Géologique de France. Deuxiéme
Série. Vol. xxu. Feuill.8-16. December 1864 to February 1865.

Ville.—Etude des puits artésiens dans le bassin du Hodna et dans le
Sahara des provinces d’Alger et de Constantine, 113.

Th. Ebray.—Sur Vage du granite syénitique du Beaujolais, 122.

Virlet d’Aoust.—Phénoménes géologiques observés dans la tranchée
de la rue de Rome, 136.

G. de Mortillet.—L’époque quaternaire dans la vallée du Pé, 188.

Virlet d’Aoust.—Flexibilité générale des couches du globe, 155.

L’abbé Pouech.—Découverte du quatriéme étage du lias dans le dé-
partement de l’Ariége, 162.

A. Boué.—Modifications d’une partie de ses classements géologiques
de la Turquie en 1840, 164.

EK. Dumortier.—Sur la Rhynchonella meridionalis et la Terebratula
Brebissom, 174.

EKug. Wolmeringer —Sur la nature et 1’épaisseur du terrain d’alluvion
de la vallée de Adour entre Hastingues et Lahonce (Basses-Pyré-
nées), 176.

G. de Mortillet.—Note additionnelle sur la vallée du Pé, 177 (plate).

56 DONATIONS, ©

Paris. Bulletin de la Société Géologique de France. Deuxiéme
Série. Vol. xxii. Feuill. 8-16 (continued). .

Melleville.—Sur les gisements de Coeuvres et de Jouy (Aisne), 180.

Virlet d’Aoust.—Nombreuses traces de marmites de géants dans le
terrain éocéne.—Phénoménes des tinaja et des tinajillas, au Mexi-
que, 186.

J. Delanotie.—Les marquois ou puits naturels, 187.

Th. Ebray.—Sur Hemiaster Vernewili en réponse aux observations
de M. Hébert, 190.

Hébert.—Etude critique sur un groupe d’ Hemiaster, 193.

-———. Sur le groupe de Bélemnites auquel de Blainville et Alc.
d’Orbigny ont donné le nom de Belemmnites brevis, 201.

L. Pareto.—Sur les subdivisions que l’on pourrait établir dans les
terrains tertiaires de l’Apennin septentrional, 210.

Comptes Rendus des Séances de l’Académie des Sciences.
Table des Matiéres du tome lix. Juillet 4 Décembre 1864.

Ramon de la Sagra.—Note accompagnant l’envoi d’une coupe figurée
des terrains traversés dans un forage pratiqué prés de la ville de
Cienfuegos, Cuba, 111.

Martin et Garrigou.—Htude géologique sur les eaux sulfureuses d’Ax
(Ariége) et sur le groupe de sources auquel elles se rattachent,
433.

Scoutetten.—Recherches sur les eaux minérales, et spécialement sur
la cause de leurs propriétés actives, 550.

Lecoq.—Note accompagnant l’envoi de son livre sur les eaux miné-
rales du massif central de la France, 651.

—. lettre sur “Les eaux minérales considérées dans leurs rap-
ports avec la Chimie et la Géologie,” 225.

Massieu.—Sur la constitution géologique des terrains traversés par le
chemin de fer de Rennes 4 Brest, 129.

De Verneuil.—Note accompagnant la présentation de la carte géolo-
gique de l’Hspagne, qwil a faite en collaboration avec M. Collomb,
417,

L. Vaillant.—Sur la constitution géologique de quelques terrains des
environs de V’isthme de Suez, 867.

Guillemin.—Mémoire sur une exploration géologique de Madagascar,
993.

Pissis.—Exploration géologique de Araucania et des ‘pays voisins,
1080. .

Des Moulins.—Lettre accompagnant un mémoire sur le bassin hydro-
oraphique du Couzeau dans ses rapports avec la vallée de la Dor-
dogne, 1085. :

Cloéz.—Analyse chimique de la pierre météorique d’Orgueil, 37.

Pisani.—Etude chimique et analyse de l’aérolithe d’Orgueil, 132.

Des Cloizeaux.—Sur la présence d’un carbonate de magnésie et de fer
cristallisé dans la météorite d’Orgueil, 829.

Daubrée.—Sur la présence de la breunnerite dans cette météorite, 830.

Cloéz.—Sur le dosage du carbone dans la méme météorite, 830.

Daubrée.—N ote accompagnant la présentation de la masse principale
des météorites tombées a l’Aigle (Orne) le 26 Avril 1803.—Cata-
logue des météorites existant en 1864 dans la collection du Muséum
d’ Histoire naturelle, 1065.

Cavaroz.—Corps d’origine météorique observés au Mexique, 1099.

Damour et H. bicOlnire Deville.—Nouvelle analyse de la Parisite,
270.

DONATIONS. oe

Paris. Comptes Rendus des Séances de l’Académie des Sciences.
Table des Matiéres du tome lix. (continued).

Pisani.—Analyse de la Langite, nouveau minéral du Cornouailles, 633.

Damour.—Sur la callais, nouveau phosphate (alumine hydraté re-
cueilli dans un tombeau celtique du Morbihan, 936.

Terreil—Analyse de diverses substances minérales du royaume de
Siam, 1047.

Boucher de Perthes.—Note relative 4 de nouveaux ossements humains
découverts 4 Moulin-Quignon, 107.

Buteux.—Sur les ossements humains d’Abbeville, 121.

Husson.—Recherches complémentaires sur les cavernes a ossements
des environs de Toul, 323.

Chevalier.—Découverte d’un nouvel atelier de fabrication d’instru-
ments en silex, 326.

Bourgeois.—Hissai de détermination des caractéres propres 4 distin-
euer les armes et instruments en silex de diverses époques, 529.
Garrigou et Filhol.— Aper¢u paléontologique sur les cavernes de l’age

de la pierre suisse, dans la vallée de Tarascon (Ariége), 593.

Gervais.—Lettre accompagnant l’envoi d’un mémoire imprimé sur
la caverne de Bize et les espéces animales dont les débris y sont
associés & ceux de l’homme, 945.

Ei. Robert.—Rapprochement entre les gisements de silex travaillés
des bords de la Somme et ceux de Brégy, Meudon, Pressigny-le-
erand, etc., dans lintérieur des terres ou bien au-dessus des grands
cours d’eau, 661.

Bourdran.—Sur deux nouveaux gisements d’armes en silex, 854.

Van Beneden.—-Sur la découverte d’ossements humains enfouis avec
des ossements d’animaux qui n’habitent plus le pays, 1087.

P. Secchi.—Instruments en silex trouvés prés d’Alatri, 548.

De Luca.—Recherches chimiques sur la composition des os décou-
verts 4 Pompei, 567.

Boesch.—Lettre concernant les météorites, silex travaillés et autres
corps pierreux désignés en Alsace sous le nom de ‘‘haches de la
foudre,” 713.

Cavaroz.—Ossements fossiles découverts en diverses parties du Mex-
ique, 1099.

Renou.—Sur un tremblement de terre ressenti & Venddme, 206.

De Tchihatchef.—Sur un tremblement de terre ressenti 4 Florence et
dans les environs les 11 et 12 décembre 1864, 1023.

Philadelphia. American Philosophical Society. Proceedings. Vol. ix.
Nos. 71 & 72. 1864.
J. P. Lesley.—Abbeville Quarries, 388 (2 plates).
Ancient Sea-level, 399.
Dubois.—Magnesium, 458.
W. A. Hendry.—Nova Scotia Coal, 459.
J. M. Hale.—Old Salt-well in Pennsylvania, 459.
J. P. Lesley.—Late Discovery of Lignite in Middle Pennsylvania, 463

(5 plates).
——. ——.. Transactions. NewSeries. Vol. xiii. Partl. 1865.
——. ——. Iistof Members. 1864.

Photographic Journal. Vol.x. Nos. 159-161. July to September
1865.

58 DONATIONS.

Presburg. Correspondenzblatt des Vereins fiir Naturkunde. Vol. u.
1863.

T. Szekecsd.—Die k.-k. geologische Reichsanstalt in Wien, 215.

EH. Mack.—Vorkommen von Lignit und Schichtenfolge beim Graben
eines Brunnens in Presburg, 191.

Ueber Petroleum, 192.

Geologische Detailaufnahme des Presburger und Neutraer Komitates
durch die k.-k. geolog. Reichsanstalt, 198.

F. Stoliczka.—Ueber das eigenthiimliche Auftreten krystallinischer
Schiefergebilde im stidwestlichen Ungarn, 76.

I’. Karrer.—Ueber das Auftreten der Foraminiferen in dem marinen
Tegel des Wiener Beckens, 78.

Aujesky.—Ueber die Verinderungen i im Salzgehalt der Ofner Elisa-
beth- und Hildegard- Bitterquellen i im Jahre 1861, 80.

Tschermak.—Untersuchung des Cancrinits von Ditro in Siebenbiir-
gen, 80.

Schaub.—Ueber die periodische Quelle bei Shae, 95.

K. Nendtvich.— Analyse der Mineralquelle von Agyagos, 114.

——. Analyse der Steinkohlen von Kis-Zello und Werolnik, 115.

J. Molnar.—Analyse der Konig Mathiasquelle, 116.

K. A. Zittel.—Geologische Verhiltnisse der oberen Nummuliten-
formation in Ungarn, 127.

Hin neuer Wolfr amit, lie

Detailaufnahmen der k.-k, geolog. Reichsanstalt in den impatient
199.

Hine eigenthtimliche Krystallform des Diamants, 204.

Schmelzung von kohlensaurem Kalk und Darstellung kunstlichen
Marmors, 233.

Posepny.—Die Quarzite von Drjtoma in Ungarn, 286.

Quarterly Journal of Microscopical Science. New Series. Vol. xin.
No. 19. July 1865.

Quarterly Journal of Science. Vol. 11. No.7. July 1865.

E. Hull.—New Red Sandstone as a Source of Water-supply for the
Central Towns of England, 418.

Chronicles of Science, 432.

W. Pengelly.—Sahara and the North-east Trade Wind, 565.

Reader. Vol. vi. Nos. 131-144. July to September 1865.

Notices of Meetings of Scientific Societies, &c.

C. W. King’s ‘Natural History of Precious Stones and of the Precious
Metals,’ noticed, 32.

W. B. Carpenter.—The Eozoén Canadense, 45.

The Glacial Period in New Brunswick, 67.

Belgian Bone-caves, 68.

J. D. Hooker—Moraines of the Tees Valley, 71.

W.S. Jevons’s ‘Coal Question. An Inquiry concerning the Progress
of the Nation and the Probable Exhaustion of our Coal-mines,’
noticed, 85.

A. Geikie’s ‘The Scenery of Scotland viewed in connexion with its
Physical Geography,’ noticed, 114.

The Archeeopteryx again, 123.

DONATIONS. 59

Reader. Vol. vi. Nos. 131-144 (continued).

A. C. Ramsay.—The Ice-drifted Conglomerates of the Old Red
Sandstone, 186.

Paleontographical Society, 207.

W. King.—Histology of Rhynchopora Geimitziana, 211.

J. Croll.—Physical cause of the submergence of the land during the
Glacial Epoch, 270.

R. G. M. Browne’s ‘ Astronomical Geology,’ noticed, 287.

Meeting of British Association, 291, 321, 349, 379.

O. Fisher.—The Glacial Epoch, 297.

S. V. Wood, jun.—The Glacial Epoch; 297.

W. B. Carpenter.—The Eozodn Canadense, 325.

H. Pratt.—Glacial Submergence, 354.

- Royal Asiatic Society of Great Britain and Ireland. Journal. New
meres, Vol.i. Part 2. 1865:

Royal Geographical Society. Journal. Vol. xxxiv. 1864.

Hi. H. Godwin-Austen.—Glaciers of the Mustakh Range, 19 (map).

J. Haast.—Mountains and Glaciers of the Canterbury Province, New
Zealand, 87 (map).

C. Forbes.—Physical Geography of Vancouver Island, 154 (map).

J. Kirk.—Fossil Bones from the Alluvial Strata of the Zambesi

Delta, 199.
R. I. Murchison.—Antiquity of the Physical Geography of Inner
Africa, 201.
J. pe, ocount of the Physical Geography of Newfoundland,
63.

—. Proceedings. Vol.ix. Nos. 3-6. 1865.

C. M. Doughty—Summer Motions of some Glacier-streams in
Southern Norway, 109.

Royal Horticultural Society. Proceedings. Vol. v. Nos. 7-9.
July to September 1865.

Royal Irish Academy. Proceedings. Vol. viii. 1864. —
J. B. Jukes.—Flint Implements found at St. Acheul, 220.

Royal Society. Proceedings. Vol. xiv. Nos. 76 & 77. 1865.
- K. W. Binney.—Description of some Fossil Plants, showing struc-
ture, found in the Lower Coal-seams of Lancashire and Yorkshire,
327.
R. Owen.—Fossil Mammals of Australia. Part II. Description of an
almost entire Skull of Thylacoleo carnifex, 343.
N. 8. Maskelyne.—New Cornish Minerals of the Brochantite Group,
392.

Shanghai. Journal of the North-China Branch of the Royal Asiatic
Society. New Series. No. 1. December 1864.

J. Henderson.—On the Physical Causes which modify Climate, 142.
Seana Report of Council. 1865.

60 DONATIONS.

Society of Arts. Journal. Vol. xiii. Nos.659-671. July to Sep-
tember 1865. |

Statistics relating to Bismuth, 598.
Mineral Statistics for 1864, 642.
Meeting of British Association, 659, 669.
Silver-mines in New South Wales, 665.
Copper-mines in New South Wales, 666.

Stuttgart. Wiirtemburgische naturwissenschaftliche Jahreshefte.
Jahrgang 21. Hefte 1-3. 1864.

Reusch.—Ueber den Agat, 55.

. Ueber den Hydrophan, 57.

Schuler.—Die Machtigkeit des braunen Jura, 67 (plate).

Schwager.—Beitrag zur Kenntniss der mikroskopischen Fauna juras-
sischer Schichten, 82 (6 plates).

Klipfel.—Geologische Mittheilungen, 152.

C. Binder. —Geologisches Profil des Hisenbahn-Tunnels bei Heil-
bronn, 165 (plate).

A. Oppel.—Ueber das Lager von Seesternen im Lias amd Keuper, 206.

Vienna. Jahrbuch der k.-k. geologischen Reichsanstalt. Vol. xv.
No.1. January to March 1865.

V. Lipold.—Das Kohlengebiet in den norddéstlichen Alpen, 1.
Verhandlungen der k.-k. “geolog ischen Reichsanstalt 1865.

Kaiserliche Akademie der Wissenschaften. Abstracts of
Proceedings. Jahrgang 1865. Nos. 16-20.

A. Boué.—Ueber die mineralogisch-palaiontologische Bestimmung
der geologischen Gebilde, 102.

EK. Suess.—Ueber die Classification der Ammoniten, 112.

F’. Stoliczka.—Hine Revision der Gastropoden der Gosauschichten in
den Ostalpen, 117.

Reuss.—Ueber die Foraminiferen, Anthozoen und Bryozoen des
deutschen Septarienthones, 126.

V. R. v. Zepharovich.—Krystallographische Mittheilungen aus den
chemischen Laboratorien zu Graz und Prag, 138.

Verhandlungen der k.-k. zoologisch-botanischen Gesellschaft
in Wien. Vol. xiv. Hefte 1-4. 1864.
G. R. v. Frauenfeld.—Zoologische Miscellen, I., 147 (plate).

Verzeichniss der Namen der fossilen mad icone Arten der
Gattung Paludina, Lam., 561.

Warwickshire Naturalists’ and Archeologists’ Field-club. Proceed-
ings. 1864.

DONATIONS. 61

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. Third Series. Vol. xvi.
Nos. 91-93. . July to September 1865.

F, M‘Coy.—Occurrence of Limopsis Belcheri, Corbula sulcata, and
some other recent Shells in the fossil state in Miocene Tertiary
Beds near Melbourne, 115.

P. M. Duncan.—Description of some Fossil Corals from the South
Australian Tertiaries, 182 (plate).

Leonhard und Geinitz’s Neues Jahrbuch fur Mineralogie, Geologie,
und Paliontologie. Jahrgang 1865. Heft 4.

H. B. Geinitz.—Ueber einige seltene Versteinerungen aus der unteren
Dyas und der Steinkohlenformation, 385 (2 plates).

Goppert.— Ueber das Vorkommen von Baumfarn in der fossilen Flora,
insbesondere in der Kreide-Formation, 395.

F, Wibel.— Die Umwandlungs-Producte alter Broncen. Hin Beitrag

_ gar Genesis einiger Kupfererze insbesondere des Kupferoxyduls,
400.

A. Streng.—Ueber die Zusammensetzung einiger Silicate mit beson-
derer Berticksichtigung der polymeren Isomorphie, 411.

Letters; Notices of Books, Minerals, Geology, and Fossils.

L’Institut. 1 Section. 33° Année. Nos. 1646-1648 & 1650-
1655; |

===) 2° Section, 30° Année.’ Nos. 357 & 358.

Natural History Review. Vol. v. No. 19.. 1865.

W. B. Dawkins.—Dentition of Rhinoceros megarhinus, 399.
J. Evans.—Portions of a Cranium and a Jaw in the slab containing
the fossil remains of the Archeopteryx, 415.

Palzontographica: herausgegeben von Hermann von Mayer. Vol.
xu. Lief.5 &6. February and June 1865.

R. Goppert.—Die fossile Flora der Permischen Formation (Fortset-
zung), 225 (24 plates).

: herausgegeben von Dr. Wilh. Dunker. Vol. xiii. Lief. 4.
August 1865.

U. Schloenbach.—Beitriige zur Palaeontologie der Jura- und Kreide-
Formation im nordwestlichen Deutschland, 147 (10 plates).

F, H. Roemer.—Die Quadraten-Kreide des Sudmerberges bei Goslar,
193 (plate). ;

ee herausgegeben von Hermann von Mayer. Vol. xiv. Lief. 2
& 3. May and August 1865.

H. von Mayer.—Fossiles Gehirn von einem S&ugethier aus der
Nieder-Rheinischen Braunkohle, 37 (plate).

R. Ludwig.—Fossile Conchylien aus den tertiaren Siisswasser- und
Meerwasser-Ablagerungen in Kurhessen, Grossherzogthum Hessen
und der Bayer’schen Rhon, 40 (12 plates).

62 DONATIONS,

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Ltalies.

Annales Hydrographiques: recueil d’avis, instructions, documents,
et mémoires relatifs a Vhydrographie et 4 la navigation. 1%, 2°, 3°,
et 4° Trimestres de 1864, et 17% Trimestre de 1865. 1864-65.
From the Dépot de la Marine.

Austin, T. The Millstone Grit, its fossils and the relation it bears
to other groups of rocks, more particularly as it occurs in the
Bristol District and South-west of England generally. 1865.

Bendyshe, T. The Anthropological Treatises of Johann Friedrich
Blumenbach. 1865. From the Anthropological Society.

Binney, W.G. Bibliography of North-American Conchology. Part
II. Foreign Authors. 1864. From the Smithsonian Institution.

Bose. Instruction pour le Micrométre Lugeol 4 Cadran Lorieux.
1864. From the Dépot de la Marine.

Burmeister, H. und C. Giebel. Die Versteinerungen von Juntas im
Thal des Rio de Copiapo. 1861. From Sir R. I. Murchison,
KOC. Bz, 0H .G Sa Oe.

Catalogue. Catalogue de la superbe bibliothéque d’Ethnographie,
de Zoologie, d’ Anatomie Comparée, etc., formée par M. W. Vrolik.
1865. From J. Gwyn Jeffreys, Esq., F.GS.

——. Catalogue of the Library of the late W. B. Baikie, M.D.,
R.N., &. 1865. From Messrs. Puttick and Simpson.

Cleghorn. Lecture on the Geology of the Surface of Caithness.
1854. From Sir R. I. Murchison, K.C.B., F.GS., &e.

Codrington, T. The Geology of the Berks and Hants Extension
and Marlborough Railways. 1865.

Combes, J.-L. Etudes géologiques sur lAncienneté de ’Homme
et sur sa co-existence avec divers animaux d’espéces éteintes ou
émigrées dans les vallées du Lot, et de ses affluents la Theze, la
Lémance, et la Léde. 1865. From Sir C. Lyell, Bart., F.GS., Se.

Couy, E. Renseignements sur la navigation des cétes et des riviéres —
de la Guyane Francaise. 1865. rom the Dépot de la Marie.

Delesse. Cartes Géologique et Hydrologique de la ville de Paris.
1861. From Sir R. I. Murchison, K.C.B., F.GS., Se.

Delesse et Laugel. Revue de Géologie pour les années 1862 et 1863.
1865.

Desnoyers, J. Réponse a des Objections faites au sujet de stries et
d’incisions constatées sur des ossements de Mammiféres fossiles
des environs de Chartres. 1863. °

DONATIONS. 63

Desnoyers, J. Surles Indices matériels de laCo-existencede l’ Homme
avec VHlephas meridionalis dans un terrain des environs de
Chartres, plus ancien que les terrains de transport quaternaires
des vallées de la Somme et de la Seine. 1863.

Desnoyers, 8S. Instructions nautiques sur les cétes de Corse. 1865.
From the Dépot de la Marie.

Dove, H.W. La loi des tempétes considérée dans ses rapports avec
les mouyements de l’atmosphere. 1864. From the Dépét de la
Marine.

Fonyielle, W.de. L’ Homme Fossile étude de philosophie zoologique.
1865. From Messrs. Bailliere & Co.

Foote, R. B. On the Occurrence of Stone Implements in Lateritic
Formations in various parts of the Madras and North Arcot
Districts. 1865.

Fournet, J. Note sur un effet de coloration des nuages observé le
9 mai 1852, 4 Ouillins. 1852.

Sur la distribution des coups de foudre 4 Lyon. 1852.
From Sir R. I. Murchison, K.C.B., F.GS., fe.

Garrigou, F. Etude comparative des alluvions Quaternaires anci-
ennes et des Cavernes 4 ossements des Pyrénées et de Vouest de
P Europe au point de vue Géologique, Paléontologique, et Anthro-
pologique. 1865,

—. Ktudes sur les Cranes de la Caverne de Lombrives. 1865.

Gastaldi, B. Lake-habitations and Pre-Historic Remains in the
Turbaries and Marl-beds of Northern and Central Italy. Trans-
lated from the Italian and edited by C. H. Chambers. 1865.
From the Anthropological Society.

Gaussin et Ploix. Annuaire des Marées des cétes de France pour
Van 1866. 1865. From the Dépot de la Marine. °

Geinitz, H. B. Das Konigliche mineralogische Museum in Dresden. -
1858. From Sir R. I. Murchison, K.0.B., F.G.S., Se.

Germain. Madagascar (Cote Orientale). Partie comprenant Vile
Fong, Tamatave, Foule-pointe, Mahambo, Fénérive, Sainte-Marie
et Tintingue. 1864. From the Dépét de la Marine.

Goeppert, H. R. Ueber die Flora der Permischen Formation. 1865.

Gras, A. le. Mer du Nord. IV®° Partie. La Tamise.—La Medway.
Les cétes de la mer du Nord, depuis le cap Gris-Nez Jusqu’au cap
Skagen. 1864. From the Dépét de la Marine.

Routier de la Cote Nord d’Espagne. 1864. From the Dépit
de la Marine.

64. DONATIONS.

Hauer, F. R.v. Bericht tiber die geologische Uebersichts-Aufnahme
im nordostlichen Ungarn im Sommer 1858. From Sir R. J.
Murchison, K.C.B., F.GS., Se.

Haughton, §.° On the Origin of Granite. 1862. From Str R. I.
Murchison, K.C.B., F.G.S., ¥e.

Hébert. Etude critique sur un groupe @Hémiasters comprenant:
Hemaaster Verneml, Desor; H. Leymeru, Desor; H. similis, d’Orb. ;
H. Fouwrneli, Desh.; et H. Orbignyanus, Desor. 1865.

——,. Observations sur la craie inférieure des environs de Rochefort
(Charente-Inférieure), 1864.

Sur le groupe de Belemnites auquel de Blainville et d’Orbigny
ont donné le nom de B. brevis. 1865.

Hitchcock, E. An account of the Ornithichnites or Foot-marks of
Birds on the New Red Sandstone of the Valley of Connecticut.
1836. From Sir &. I. Murchison, K.C.B., F.GS., fe.

Jukes, J. B. Notes for a comparison between the Rocks of the -
South-west of Ireland and those of North Devon, and of Rhenish
Prussia (in the neighbourhood of Coblentz). 1865.

Kerhallet, E. P. de. Manuel de la navigation dans la Mer des An-
tilles et dans le Golfe du Mexique. 3° Partie. 1864. From the
Dépot de la Marine.

Kokscharow, N.v. Mineralogische Notizen. From Sir R. I. Mur-
chison, K.C.B., F.GS., Se.

Ueber den Russischen Monazit und Aeschynit. 1861. From
Sir R. I. Murchison, K.C.B., F.GS., &£e.

Lartét, L. Sur la Formation du bassin de la mer Morte ou lac
Asphaltite et sur les changements survenus dans le niveau de ce
lac. 1865. From Sir C. Lyell, Bart., L.GS., Se.

Lartét, E. Sur une ancienne station humaine, avec sépulture con-
temporaine des grands Mammifcres fossiles réputés caractéristiques
de la derniére période géologique. 1861.

Ledough. Nuage orageux observé sous le point culminant de ~
V’Edough prés de Bone. 1853. rom Sir BR. I. Murchison, K.C.B.,

F.GS., Fe.

Lentillac, E. de., et Z. Guclbert. Rapport sur la Double présenté
3 la Société d’Agriculture, Sciences et Arts, et 4 PAssociation
Médicale de la Dordogne. 1863. .

Lesley, J. P. Note on a new Lignite-deposit, discovered near the
Pond-bank of Mont Alto Furnace, Franklin County, and on its
relation to the question of the date of the Appalachian Chain.

1865.

DONATIONS. 65

Lesley, J. P. Petroleum. Geological Report on Lands on Paint
Lick Fork of Sandy River, in Eastern Kentucky. 1865. From
Sir C. Lyell, Bart., F.GS., Se.

Le Verrier, U. J. Service Météorologique des Ports. Lettre a M.
Airy, Astronome Royale d’Angleterre. 1860. From Sir R&. J.
Murchison, K.C.B., F.G.S., &e.

Locke, J. On the Antiquity of Man. 1865.
MacDermott. Instructions Nautiques pour les principaux ports de

la cote est de Amérique du Nord. 1864. rom the Dépét de la
Marine.

Matteucci, C. Electro-Physiological Researches. 4th memoir. The
Physiological Action of the Electric Current. 1846. From Sir
R. I. Murchison, K.C.B., F.GS., fe.

Meek, F.B. Check-list of the Invertebrate Fossils of North America.
Miocene. 1864.

: . Cretaceous and Jurassic. 1864. From the Smth-
sonian Institution.

Montagna, C. Generazione della Terra metodicamente esposta con
-nuoyi principli di Geologia. Fasc.5 & 6. 1865. From Sir C.
Lyell, Bart., F.GS., Sc.

Moore, C. On the Zones of the Lower Lias and the Avicula-contorta
Zone. 1861. From Sir R. I. Murchison, K.C.B., F.GS., fe.

Morgan, A. de. Contents of the Correspondence of Scientific Men
of the 17th Century. 1862. From Sir R. I. Murchison, K.C.B.,
aEG US... ie.

Mortillet, G. de. L’époque quaternaire dans la valleé du P6. 1864.

Les Mystifiés de ’ Académie des Sciences, défi adressé 4 MM.
Decaisne et Elie de Beaumont. 1865.

Murchison, R. I. Address to the Geological Section of the British
Association at Birmingham. 1865.

Parker, W. K., T. R. Jones, and H. B. Brady. On the Nomen-
clature of the Foraminifera. Part xii. 1865.

Perthes, B. de. Antiquités Celtiques et Antédiluviennes. Mémoires
sur l’industrie primitive et les arts 4 leur origine. Vol. iii. 1864.

Ponzi, G. Storia Naturale dell’ Agro Pontino. 1865. From Sir
C. Lyell, Bart., F.GS., Se.

Pouchet, G. The Plurality of the Human Race. Translated and
edited by H. J. C. Beavan. 1564. From the Anthropological
Society.

Quetelet, A. Histoire des Sciences Mathématiques et Physiques chez
les Belges. 1864.
VOL. XXII.—PART I. F

66 DONATIONS.

Quetelet, A. Observations des Phénoménes Périodiques des plantes
et des animaux pendant les années 1861 et 1862. 1862.

——. Paroles prononcées lors des funérailles de M. Jean Kickx.
1864.

——. Sur la Statistique générale des différents pays. 1861.

——. Sur le systéme décimal. 1861. From Sir R. I. Murchison,
KCCLB OE .G Sa Gie:

Recherches sur les Chronomeétres et les Instruments Nautiques.
Part VII. 1864. From the Dépét de la Marine.

Report. Annual Report of the Trustees of the Museum of Compa-
rative Zoology at Harvard College, in Cambridge, together with
the Report of the Director, 1864. 1865. .

Quarterly Report of the Meteorological Society of Scotland ;
for the quarter ending December 31, 1859. 1860. From Si
KR. I. Murchison, K.C.B., F.GS., &e.

Report of the Director of the Geological Survey of Victoria
for the period from June 1863 to September 1864, with Appen-
dices. 1865. From A. R. C. Selwyn, Esq.

Report of the Progress of the Geological Survey of Canada
for the year 1852-53. 1854. From Sir R. I. Murchison, K.C.B.,
POG Ses ies

Report of the Trustees of the Montreal Mining Company to
the Shareholders. 1846. From Sir R. I. Murchison, K.C.B.,
JER Si Gi

——. Results of Meteorological Observations made under the
direction of the United States Patent Office and the Smithsonian
Institution, from the year 1854 to 1859, inclusive, being a Report
of the Commissioner of Patents made at the First Session of the
36th Congress. Vol. 11. Part 1. 1864. From the Smithsonian
Institution. :

——. Second Report of the Commissioners for the Exhibition of
1851, to the Right Hon. 8. Horatio Walpole. 1852.

——. Third Report of the Commissioners for the Exhibition of
1851, to the Right Hon. Sir George Grey, Bart. 1852. From
Sir R. I. Murchison, K.C.B., F.GS., §.

Reuss, A. H. Zur Fauna des deutschen Oberoligocins. 1864.
—-. Zwei neue Anthozoen aus den Hallstadter Schichten. 1865.
Romanofski, G. On Geological Researches in Central Russia. 1863.

Schvarez, J. A Gorogok Holdja pericles koraban s valami a demo-
eritféle tejatrol. 1861. From Sir R. I. Murchison, K.O.B.,
F.GS., Sc.

DONATIONS. 67

Sella, Q. Sulle forme cristalline di alcuni sali derivati dall’ Ammo-
niaca. 1861. From Sir R. I. Murchison, K.C.B., F.GS., Fe.

Silliman, B. Address before the Association of American Geologists
and Naturalists. 1842. From Sir R. I. Murchison, K.C.B.,
F.GS., ¥e. :

: Consistency of the discoveries of Modern Geology with the
Sacred History of the Creation and the Deluge. 1833. From
Sir R. I. Murchison, K.C.B., F.GS., Se.

Sismonda, E, Appendice alla descrizione dei Pesci e dei Crostacei
fossili nel Piemonte. 1861. From Sir R. I. Murchison, K.C.B.,
#G.S., Sc.

Smith, E. Experimental Inquiries into the Chemical and other
Phenomena of Respiration, and their Modifications by various
Physical Agencies. 1859. From Sir hh. I. Murchison, K.C.B.,
F.G.S., ge.

Smithsonian Institution. Smithsonian Contributions to Knowledge.
Vol. xiv. 1865.

Staring, W.C.H. Over de herkomst van het Grind Onzer Rivieren.
From Sir R. I. Murchison, K.C.B., F.GS., &e.

Suess, H. Ueber die Cephalopoden-Sippe Acanthoteuthis, R. Wagn.
1865.

Torell, O. Bidrag till Spitsbergens Molluskfauna jemte en allmin
ofversigt af Arktiska Regionens naturforhallanden och forntida
utbredning. I. 1859. From Sir R. I. Murchison, K.C.B.,
F.GS., &.

Unger, F., K. Zittel, E. Suess, F. Karrer, F. Stoliczka, und G. Jaeger.
Paliontologie von Neu-Seeland. Beitrage zur Kenntniss der fos-
silen Flora und Fauna der Provinzen Auckland und Nelson. 1865.
From Dr. F. von Hochstetter.

United States. Statistics of the Foreign Commerce of the United
States; embracing a historical review and analysis of foreign
commerce between the Mississippi and Atlantic States; the over-
land trade and communications with the Pacific States; the pro-
ductions and exchanges of the Gold- and Silver-districts ; the com-
merce of the Pacific coast, and the International Relations of the
Northern Frontier of the United States. 1864. From the Smith-
sonian Institution.

Vancouver Island. Report of Exploration. 1864. From Robert
Brown, Esq., Commander.

Victoria. Gold-fields’ Statistics. 1861. From Sir R. I, Murchison,
K.C.B., F.GS., Se.

Vogt, C. Lectures on Man: his Place in Creation and in the History
of the Karth. Edited by J. Hunt. 1864. From the Anthropo-
logical Society.

68 DONATIONS.

Volborth, A. v. Ueber die mit glatten Rumpfgliedern versehenen
Russischen Trilobiten. 1863. From Sir R. I. Murchison, K.C.B., .
F.GS., Se.

Waagen, W. Versuch einer allgemeinen Classification der Schichten
des oberen Jura. 1865.

Winkler, T. C. Musée Teyler. Catalogue systématique de la Col-
lection Paléontologique. Troisiéme livraison. 1865. From Sir

C. Lyell, Bart., F.GS., Se.

Wood, S. V., jun. Remarks in explanation of a Map of the Upper
Tertiaries of the Counties of Norfolk, Suffolk, Essex, Middlesex,
Hertford, Cambridge, Huntingdon, and Bedford, with parts of
those of Buckingham and Lincoln, and accompanying Sections.
1865.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCHEDINGS

OF

THE GEOLOGICAL SOCIETY.

_ Drcemser 6, 1865.

W. Phipson Beale, Esq., 27 Victoria Street, S.W.; Henry Brad-
don, Esq., 5 Danes’ Inn, Strand; Captain Robert Clipperton,
H.B.M. Consul at Kertch; Tellef Dahll, Esq., Kragere, Norway ;
R. A. Eskrigge, Esq., 24 The Albany, Old Hall Street, Liverpool ;
Hugh Frederick Hall, Esq., Liverpool; Hedworth Hylton Joliffe,
Ksq., Merstham, Surrey; Edward Myers, Esq., 29 Summer Hill
Terrace, Birmingham ; George Pycroft, Esq., M.R.C.S.E., Kenton,
Exeter; Ferdinand Stoliczka, Ph.D., of the Geological Survey of
India, Caleutta; Erwin Harvey Wadge, Esq., Stradbrook Hall,
Blackrock, co. Dublin, Ireland; Henry Augustus Ward, Esq., Pro-

fessor of Natural Sciences in the University of Rochester, New York ;
- and Frederick M. Williams, Esq., M.P., Goonvrae, near Truro, were
elected Fellows.

The following communications were read :—

1. On the Western Litt of the Raaric Bens in Soura Wats, and
on the Posrrion of the “ Surron Stonz.” By E. B. Tawney, Esq.,

F.G.8. With a note on the Corats, by P. Martin Duncan, M.B.,
Sec.G.8.

[Puates IIT. & IV.]

ConTENTS.
1. Introduction. 8. Position of the Sutton Stone.
2. Pyle district. 9. Middle Lias.
3. Bridgend district. 10. Table showing the range of the
4. Keuper near Bridgend. fossils of the Rheetic beds of
5. Sutton Stone. South Wales.
6. Sutton Series. _ 11. Descriptions. of the species.
7. Southerndown Series.

1. Introduction.—The object of the present paper is to notice some
VOL. XXII.—PART I. G

70 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Dec. 6,

peculiarities of the Avicula-contorta series at their most westerly
boundary in Great Britain; to discuss the “Sutton Stone” as to its
stratigraphical, lithological, and paleontological relations; to show
from organic remains that its affinities are with the Triassic forma-
tion, and not with the Lias as commonly supposed, and then to claim
it as Rheetic, and in so doing to extend, for the first time in England,
the range of Ammonites down into the Rheetic series.

At the Bath Meeting of the British Association for 1864, Sir R.
I. Murchison announced the presence of the argillaceous limestones
and shales of the Rheetic series ina small outlier of Lias (as mapped)
close to Pyle Station (west of Bridgend) ; and having in this way had
my attention directed to the subject, I found that the Avicula-contorta
strata were widely extended in this district; and as they show some
peculiarities here, I will begin by a few remarks on these beds.

2. Pyle district—The above-mentioned patch, sufficiently described
by Mr. Bristow*, consists of buff-coloured marls and greyish-brown
shales and limestones, which last, from their appearance and con-
choidal fracture, remind one of the Cotham marble: these are pro-
bably high in the series ; they are mapped as lying on the Keuper.

A few hundred yards south of this we reach the southern limit of
the Keuper in this district. It consists of red marls with buff and
green marls resting upon them; the same conditions occur at the
base of the Rheetic series at Wenvoe, Barry Island: and besides this,
there is very little of the New Red series in this district; what has
been hitherto called Keuper is much of it Rheetic.

I am obliged to dissent from the opinion expressed by Sir H. De la
Beche in his comprehensive and admirable memoir on the ‘‘ Forma-
tion of Rocks in South Wales’’+, that the sandstones near Pyle church
are inferior to the red marl lately spoken of: the district is more
broken by faults than is expressed in the map of the Geological
Survey; and this may have caused some ambiguity.

The sandstones at the base (10-12 feet thick) are in places much
weathered, the iron being changed to peroxide, and the mass crum-
bling to rusty sand under the hammer; others are unoxidized and
harder, namely the pale-green or yellow thick sandstones, affording
when dry a good building-stone: some of these beds are very similar
to the white Keuper sandstones near Bridgend. Above these are hard,
green-and-white mottled and purple marls. These belong to the
Avicula-contorta series, and not to the Keuper. The search for fossils
is frequently unsuccessful here, from the oxidation of the beds, due
to exposure to moisture and air. On the quarry-refuse heaps are
found great numbers of a small species of Matica crowded together
by hundreds; Anata precursor also is abundant. The fossils of
these sandstones, which are exceedingly fossiliferous on Stormy
Down and near Laleston are

Myophoria postera, Saurichthys apicalis, Axinus elongatus,
Natica Pylensis, Acrodus minimus, depressus,
Anatina precursor, Avicula contorta, cloacinus.
Modiola minima,

* Report Brit. Assoc. Bath, 1864, Trans. Sections, p. 50.
+ Memoirs of the Geological Survey, vol. i. p. 252.

=

1865. ] TAWNEY—RHZTIC BEDS AND SUTTON STONE. v1

Since commencing this paper, a pit sunk for sand on Stormy Down
revealed the following section (this excavation has since been again
partly filled up):—At the base were seen 6 feet of the pale-green
and white sandstones; these were extremely fossiliferous (a speci-
men from these beds is presented to the Society): above were green
laminated marls containing Avicula contorta, and then yellow sands
and sandstones (about 6 feet).

3. Bridgend district.—Though fossils were perfectly conclusive as
to the true nature of the above beds, yet the following section 1s of
great interest as showing their relation to the Rhetic shales and bone-
bed. This section is on the south side of the South Wales Railway-
eutting at Cwrt-y-Coleman, about a mile and a half west of Bridgend.

At the base are seen 8 or 10 feet of white or yellowish massive
sandstone with a few small rounded quartz pebbles. I have not
found fossils in this bed, except coprolites at the top of it, but
I believe it may be of Rheetic age ; and it is probable that it will be
found to be fossiliferous, as it contains brown stains and marks of
organic matter, and in this and general structure is like some of
the beds at the top of the section. It may probably be of these
sandstones that Sir H. De la Beche notices travelled blocks on the
western part of Newton Down*; he describes it as a quartz rock
(between Pyle and Bridgend), with the grains of white ane firmly
bound together by nearly colourless silica.

Above this are about 3 feet of shales, including a curious marly
limestone, grey and green in colour, the grey part of which is very
full of shells and shell-fragments: the fracture of this bed is con-
choidal, so that the shells are nearly always broken across. Above
this is a siliceo-micaceous limestone from 2 to 3 inches thick, with
irregular marly surfaces: this is the true representative of the Aust
bone-bed. On splitting off the exterior lamin of this bed a multi-
tude of teeth of Acrodus and Hybodus and fish-scales are seen. I
haye also found a reptilian bone. The remains I have noticed in
this bed are

Saurichthys apicalis, Gyrolepis tenui- | Hybodus cuspidatus (4g.),
acuminatus, striatus, orthoconus (Plien.),

Acrodus minimus, alberti, plicatilis (4g.),
acutus, Hybodus minor (4g.), and scales of other species.

This bed is not conglomeratic, beyond an occasional rolled quartz
pebble, but is a fine-grained tough micaceous limestone.

I was ignorant at the time of this discovery that the bone-bed had
been found so far west as St. Hilary, nine miles east of Bridgend.

Above the bone-bed come dark shales, 3 feet; then a chocolate-
coloured soft sandstone-bed (1 inch) containing Avicula contorta, Pec-
ten Valoniensis ; then shales, 3 inches; then three beds of siliceous
limestones with fish-scales, Anomia, &c.; these beds change their
conditions somewhat at different parts of the section, being more
sandy in places or again thin out into shale; above are 9 feet of
shales, marls, and sandstones; and then 17 feet of white and pale-
green and yellow sandstones and sands.

* Loe, ett, p. 252.
«2

72 PROCEEDINGS OF THE GROLOGICAL SOCIETY. [ Dec. 6,

These beds represent the black shales and argillaceous limestones
above the bone-bed at Penarth, &c.

The abundance of silica and comparative scarcity of calcareous and
aluminous matter here, as compared with the sections of Penarth or
the west of England, is noticeable ; the explanation no doubt lies in
the proximity of this series to or upon the Paleozoic rocks of Car-
marthenshire, Brecknockshire, Cardiganshire, and North Wales, with
their sandstones and grits.

Though a fault is now the boundary of the Rhetic series north-
wards, it perhaps nearly corresponded with the shore of the Rheetic
sea, the rivers running into which drained large Paleozoic areas.
That the water was shallow is probable from the varied conditions of
the bedded sandstone in a small area round this district ; moreover
the abundance of sand and not mud shows the probable deposition
near a shore. That it coincided with some shore and system of
islands at the close of the Bunter period we know from the disposi-
tion of the Magnesian Conglomerate in this area. |

We may suppose that there has been no great extension either of
the Rhetic or Keuper series northward on the Coal-measures ; or .
more cases similar to that described by Sir H. de la Beche near
Bridgend, of Trias resting on Coal, would have occurred. The great
denudation of the Coal-measures took place before the deposition of
the secondary rocks here; and perhaps denuding forces have been
comparatwely passive since.

4, Keuper near Bridgend.—_North of udeeud one mile and a half
on either side of the river Ogmore, are white Keuper sandstones
showing very similar characters to some of the Avicula-contorta
sandstones: these yield a stone well fitted for architectural purposes,
being soft but durable. At the quarry here there are 25 feet of pale-
green or white Keuper sandstones capped by 6 feet of green sandy
marls (Rhetic?). These sandstones must be at the base of the
Keuper.

5. Sutton Stone.—I come now to the consideration of the Sutton
Stone. This is spoken of by Sir H. De la Beche* as a “ whitish
variety of the Lias.” He notices that it commences with a white
conglomerate enclosing pebbles of Carboniferous Limestone, upon
which formation the Sutton Stone is seen to lie, and particularly
well on the coast between Sutton and West farmhouses, and again
at Dunraven Point. He notices the grey Lias above these beds, and
draws attention to the conglomeratic character of the Lias around
Langan.

These beds I now claim as Rhetic, and would unquestionably
separate from the Lias. As developed on the coast, they are between
80 and 90 feet in thickness: to the lower half of this the term
“Sutton Series’? may apply; and for the upper half I propose the
name of ‘‘ Southerndown series,” as they are best seen in the fine
cliff-exposure under the hamlet of Southerndown.

6. Sutton Series.—The term “Sutton Stone ” is generally applied
to the white and softer beds or freestones which are used for architee-

* Loe. cit. p. 272.

1365. ] TAWNEY—RHATIC BEDS AND SUTTON SLONE. 73

tural purposes. The beds differ much in texture: some are fine-
grained white limestones, others are softer and very shelly ; some are
yellowish-white, and at the upper part are pale-grey and become gra-
dually harder. All these, together with the white conglomerate at the
base, I include in the Sutton series: the characters of whiteness and
softness are only gradually lost, the pale-grey beds being equally
fossiliferous, and in fact the top beds differ only by being darker
and harder.

The Sutton series is seen lying on the Carboniferous Limestone
along the coast from the mouth of the river Ogmore to the Southern-
down cliffs, and is again brought up by a fault at Dunraven, where it
forms the Point arching over the Carboniferous Limestone. Between
Sutton and West the Carboniferous Limestone is approximately hori-
zontal; and there is apparent conformability between it and the
white conglomerate which begins the Sutton series; further on
towards Southerndown the Carboniferous Limestone dips at about an
angle of 45°, while the Sutton series is still nearly horizontal : this is
also the relation of the beds at Dunraven Point; immediately after
this the Sutton and Southerndown series disappear beneath the Lias
and the sea.

The conglomerate at the base consists of rolled pebbles of Car-
boniferous Limestone very numerously imbedded with occasional
pieces of chert in a soft, fossiliferous, white matrix. The fossils
most abundant in this bed are

Lima tuberculata, Ostrea leevis,
Plicatula intusstriata, Cardita rhomboidalis,
acuminata, Corals,

The included fragments of Carboniferous Limestone are seen to con-
tain Spiifere, Producte, &c.

Some of the corals may be derived from the Carboniferous Lime-
stone, for that formation here is seen to be full of corals weathered
out on the surfaces of the beds by the action of the sea and at-
mosphere ; the other species are not derived. This conglomerate
is 4 feet thick. :

Above this come the white and pale-yellow freestones ; many of
these beds contain shattered fragments of black chert, frequently col-
lected together in bands. The source of these abundant chert-masses
is probably the Carboniferous Limestone. At Dunraven Point the
Carboniferous Limestone is seen to contain bands of this black chert as
well as large ramifying spongiform masses. Another noticeable
character of the series is the curious sutural junction of many of the
beds, the appearance being of miniature basalt-like columns, pro-
ceeding from a few inches deep in one bed upwards for the same
height into that immediately above ; this is, doubtless, of stalactitic
origin; the structure may sometimes be seen passing through a
fossil and distorting it more or less.

The presence and dissemination of Galena through these beds is
also to be noticed. Sir H. De la Beche notices it as occurring in
the plants of the Lower Lias (stc) here * ; this may probably be in

* Loc. cit. p. 273, in note.

74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ DeexG;

the lignite associated occasionally with the Sutton and Southern-
down series, as I believe the Galena is confined almost entirely to
these beds ; it occurs in disseminated crystals and small strings, but
not in workable veins.

It is plentifully scattered at Sutton and along the coast, and has
before been noticed at Candleston *, where an attempt was made to
work it. A more recent failure is that of Langan: a shaft was
sunk and buildings half erected before the attempt was abandoned ;
this shaft passes through parts of the grey scries, showing the rock
to be a fine conglomeratic mixture of small fiint-fragments with cal-
careous matter, and it reaches to the white series.”

These beds are very fossiliferous; I have obtained from them
some species new to Britain, and others, which are described in the
sequel. Owing to the porous nature of the rock, the original shell-
substance of the fossils is often dissolved away ; this has added much
difficulty to the determination of the species.

The most characteristic and common fossils are Pecten Suttonensis,
Ostrea multicostata, a Muschelkalk species, Lima tuberculata, a
coral, Patella Suttonensis, Plicatula intusstriata, and P. acuminata.

The Sutton Stone was formerly apparently more appreciated as a
building-stone than it is now; it was used in several Norman castles
in the county, having been conveyed considerable distances by land:
it was also used in Neath Abbey (the characteristic fossils may be
seen in stones lying about the ruins), and, I am told, in Swansea
Castle ; to these it was, no doubt, taken by water.

Besides the Sutton quarries, which are still worked, there is a
good quarry east of Tythingstone church which has not been used
for a long time, but from which much good stone has been taken.

7. Southerndown Series.—As the term Sutton Stone is applied only
to the building-stones, I have divided off the rest of the series which
intervenes before the commencement of the Lias here ; and, for con-
venience of reference, I call it the Southerndown series; this has
hitherto been regarded as Lias.

At the base we have a bed of chert- Pavel or rough shale full of
small fragments of chert, together with larger pieces; it is 9 inches
thick. This physical line may be also aaa to separate the softer,
more fossiliferous, and whiter beds below, from the harder, darker,
and perhaps less fossiliferous beds above.

As this series is not worked at all on the coast, nor much quarried
inland, our knowledge of its fossils is much less full; however,
Plicatula intusstriata occurs throughout it.

This series differs lithologically trom the Sutton Stone in the
beds being much harder and more irregularly bedded, and they are
frequently subcrystalline and separated by thin arenaceous part-
ings; again, the fragments of black chert are more sparingly scat-
tered. On the other hand, it differs from the Lower Lias beds—
which are earthy limestones separated generally by argillaceous
shales, having no fragments of black chert, and not being conglo-
meratic. The two series differ also entirely in their fossils.

* Loc. cit. p. 273, in note.

1865. | TAWNEY—RHZTIC BEDS AND SUTTON STONE.

Fig. 1.— Vertical Section of Southerndown C lif.

=a
[a ao
zZ — Am. Conybearii.
: ———) Gryphea incurva. Grey argillaceous
— limestones and
E==

= Pholadomya glabra. shales.
Am. Bucklandi.

Zone of Ammonites Buck-
landi, 20 ft. 2 in.

Pale smooth argillaceous limestone.
wees. Coarse granular shale, with cherts.

-——_—_——-

Zone of Ostrea liasstca, 9 in.

occasional partings. Lignite.

Dark-grey crystalline limestone (occa-
sional fragments of black chert).

a Granular parting, with chert frag-
| ments:

Hard grey tough limestones (blac
ee chert in places). Pinna. :

Grey limestones, with very thin part-
ings.

-\ Irregular hard grey limestones.

Sscarssavisrecsccera Coarse granular shales and fine con-
glomerate.

Hard grey granular beds.
Pale-grey shelly beds.

White or pale-yellow soft lime-
4+ stones, shelly.

Southerndown series, 50 ft. 9 in.
——$—$—<——$—$——$
\il {| ti
| r] i |
} | |

!
2
3
S;
v
iS

Fine-grained white limestones,
with bands of chert at intervals.
Discina Suttonensis, Modiola,

Lima planicostata, Cardinia

Suttonensis, Pecten Suttonen-

sis, Ostrea multicostata, Car-
| dita.

Conglomeratic band of chert.

Sutton series, 39 ft. .
Ce Oe

White conglomerate.

t SSS Coarse white conglomerate, with
Soa one r—to-, . :
\ Sabewsetg coe sue Carboniferous Limestone peb-
PS Ft BP
bles.

Fig. 2.—Coast-section from Sutton to Dunraven.

Dunraven.

Southerndown.

CaN

~SOssaceyod

eeFt ©,g0 ae

Kuls)s:91818)9)y ae
el ee | poo

eer

(Yeah 5
.
antes

2

ware en =

mfaa

* High-water level.
t Low-water level.

|

e. Carboniferous limestone.

d. Sutton series.

c. Southerndown series.

|

a. Zone of Ammonites Bucklandi.
6. Zone of Ostrea liassica.

76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Dec. 6,

Sometimes among the beds of this series may be seen a paler, softer,
and shelly bed, showing a sort of return to the conditions of the
lower beds.

This series I have estimated as 50 feet thick, having measured
it bed by bed along the coast west of Dunraven ; it extends here a
distance of about one mile and a half, forming low anticlinals, but
dipping on the whole east of south. There is some uncertainty in
this estimate, from the presence of three small faults, for which I
have allowed 43, 44, and 84 feet Herren the downthrow being
to the east.

About 16 feet down occurs a bed with a great number of large
Chemnitzie; the wearing action of the sea has formed sections
through the columella: of many, as they lie horizontally imbedded in
the limestone.terrace below high-water mark. . Owing to the hard-
ness and toughness of the beds, I have been unable to obtain spe-
cimens.

The uppermost bed of the series, which I take as the line of
demarcation from the Lias, is a bed of conglomerate composed of
chert-gravel with arenaceous matter, 4 to $ inches thick, loosely
held together ; the fossils of this bed are

Plicatula intusstriata (abun- Ostrea liassica,
dantly), Pentacrinus,
Modiola minima, Cidaris-spines.

Ostrea levis,

Above this boundary-parting is a bed of smooth, pale-grey, con-
choidal limestone, containing

Ostrea liassica, Modiola minima.
Pholadomya glabra,

Above this begins the Ammonites-Bucklandi series (the Planorbis-
beds being absent) with shale and argillaceous limestone containing
Gryphoa imeurva, My yacites unionides, Cidaris (the same as that
occurring at the top of the Rheetic series, and probably Cidaris
Edwardsi).

Then, about 3 feet up, Gryphea incurva occurs socially in dozens,
with Ammonites Conybeari, A. rotiformis, A. Bucklandi, Lima,
Pholadomya ambigua, &c.

At Dunraven Point the Carboniferous Limestone dips at an angle
of 43°, while the Sutton series lies in a gently curved arch upon
it. The Sutton series here is 40 feet thick, the same thickness as
near West, but the grey. or Southerndown series is scarcely one
quarter of its former thickness ;° there is a small fault here also.

The chief fossils which I have found in the Southerndown beds
are

Plicatula intusstriata, Pecten Suttonensis,
acuminata, Lima Dunravenensis,

Ostrea multicostata, Pinna papyracea,

Ostrea laevis, Inoceramus Ramsayi.

hese are enumerated in a tabular list as they occur in some of the
chief localities of this district (see infrd, p. 79).

1865. ] TAWNEY—RHZTIC BEDS AND SUTTON STONE. rar

8. The position of the Sutton Stone.—Having been struck by the
presence of Plicatula wtusstriata in the Sutton stone, a shell ac-
knowledged to be characteristic of the Rheetic series, and never, I
believe, really found out of it*, I convinced myself by diligent
search that the usual Liassic species of Ammonites, &c., were ab-
sent from these beds, while those fossils that were present had many
of them either been noticed in the Rhetic beds of the Continent or
showed strong affinities to the Upper Triassic fauna. This part of
the series was therefore no longer to be considered Liassic.

It now became necessary to find the boundary between the
Rheetic and Liassic series. By examining the range of the charac-
teristic species, Ostrea multicostata and Pecten Suttonensis, I observed
that they ceased vertically at a line generally marked by ltho-
logical characters.

The Southerndown series as here restricted must therefore be
taken from the Lias. The sections seen in the valley between Bridgend
and Pyle, and through which the South Wales Railway runs, are
perfectly conclusive as to the non-Liassic nature of the white or
Sutton series.

Near Cwrt-y-Coleman, &c., we find 7 feet of white shelly lime-
stones covered by 4 feet of mottled green and yellow marls, and
2 feet of purple-red marls. In the Sutton limestone here, Myo-
phoria postera is found with Turritella and other shells, of which
I have only bad specimens. The marls are Rhetic, and are very
similar to those noticed near Pyle church; they may be, perhaps,
the same as occur at the base of the “Stormy Lime and Cement
Works,” on the South Wales Railway.

At the base of these works are 9 feet of dark and pale-green mars ;
above are the Avicula-contorta shales (15 feet), with Pecten Valo-
niensis, &c.; above this are pale-grey, smooth limestones, sepa-
rated by dark brown-grey shales, which are the equivalents of the
White Lias of the West of England. The fossils here are fish-
scales and the following shells :—

Monotis decussata, Plicatula intusstriata,
Modiola minima, Ostrea liassica,

and a Cardinia, which also occurs in the White Lias of Saltford.

Above are argillaceous limestones, with Ostrea Kassica and Mo-
diola minima. The Ostrea-series is well developed in the neigh-
bourhood.

Another interesting section is seen half a mile north of the last,
at French Quarry. The Rheetic series here consists of white shelly
limestones and green marly bands. Monotis decussata and Axinus
cloacinus are very abundant; and Ostrea liassica is seen to begin
here in the Rheetic beds, and gradually increase in numbers until
it reaches its climax in the “ Ostrea-beds ” (Lower Lias).

Again, in Laleston-churchyard Quarry part of the Sutton lime-

* JT have lately heard that Plicatula intusstriata has been found attached to
Gryphea incurva from the Ammonites-Bucklandi beds. I have not, however, seen
the specimen.

78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 6,

stones are seen beneath the Monotis-beds, Monotis decussata being
characteristic in the West of England of a zone near the top of
these beds. .

In the shales here occur the spines and portions of the test of an
Echinoderm (Hemipedina?): the same species occurs at Stormy.
The presence of cubic crystals of Galena in the shales is also note-
worthy. This same section may be seen also north of Bridgend, on
the Tondu road.

It will be seen from the foregoing sections how varied are the
conditions of the Rhetic series within a small area. The Pyle
valley, enclosed between the two east and west faults mentioned by
Sir H. De la Beche*, is much broken by lesser faults; and to these
is, no doubt, due the fragmentary nature of the evidence as to the
sequence of the beds. I am unacquainted with any section which
shows the position of the Avicula-contorta sandstones in relation to
the Sutton and Southerndown series.

We have seen that some of the Sutton limestone appears to be
below the Monotis-beds, which contain also Aaimus elongatus; they
are also below green and purple marls (page 77 supra). If the green
marls in the Stormy cement-works’ section be the same as those
mentioned near Cwrt-y-Coleman, &c., we have a key to the posi-
tion of the Sutton limestones ; they would be below shales containing
Avicula contorta. We still, however, require the exact relation of
the Southerndown to the Avicula-contorta series.

We have yet to consider the evidence of fossils. And, first, the
absence of Avicula contorta from the Sutton series (a shell which is
found everywhere, in sandstones, limestones, and shales) would seem
to point to more than a mere change in the sea-bottom—namely, to
a different horizon in time. Moreover we can scarcely consider the
Sutton and Avicula-contorta series contemporaneous, as they are found
in close proximity. I believe it probable that the Sutton series was,
at any rate, slightly anterior in time to the Avicula-contorta series.
This seems likely from its physical aspect and the abundance in the ©
former of Ostrea multicostata, a characteristic Muschelkalk species,
but which has been noticed from the Infralias of Luxembourg by
Terquem; while, on the other hand, the abundance of Plicatula wm-
tusstriata, the affinities of the Pectines, Lime, and Cardinie, show
that it must be included in the Rhetic series. The presence of
Ammonites is very remarkable: there seem to be two species pre-
sent, at any rate. My specimens, however, are very imperfect.
The great paucity, if not entire absence, of Brachiopoda, as com-
pared with the foreign beds, is also remarkable. The Sutton beds
cannot be regarded as equivalents of the White Lias of the West of
England.

The Southerndown series seems to have been formed under much
the same circumstances as that of Sutton, but in deeper water in
an area of depression upon the Carboniferous Limestone of this area.
The same is the case also with the analogous beds on Broadfield
Down, near Bristol, whose similarity of condition was noticed by

* Loe. cit. p. 238.

1865.] ‘TAWNEY—RHZXTIC BEDS AND SULTON STONE. 79

Sir H. Dela Beche*. I have no doubt that these beds are also
Rhetic; they are conglomeratic in places, enclosing Carboniferous-
limestone fossils ; and they are precisely similar to the Sutton con-
glomerate. I have found in them Plicatula intusstriata, a Cardima
like the one at Stormy (page 77 supra), and an Arca abundantly as
casts. Except Ostrea liassica(?) and Modiola minima(?), the Lias
fossils seem absent.

I am greatly indebted to my friend Mr. W. Saunders, F.R.8., of
Bristol, for the inspection of his collection from the curious white
and siliceous modifications of Lias (spoken of by Buckland and
Conybearet) at Chewton Mendip, East Harptree, Shepton Mallet, &c.

An examination of these fossils leaves no doubt on my mind

that they are for the most part Rhetic; some of them were—
From Chewton, Ostrea multicostata, From Shepton { Pecten Suttonensia,

Mendip, and 4 Monotis decussata, Mallet. Tita faberanlate:

East Harptree. | Axinus elongatus.

9. Middle Inas.—As it is not expressed on the map, I may remark
that the upper part of the Bridgend Railway-section is Middle and
not Lower Lias. This is shown by the presence of Ammonites spt-
natus, Gryphaa cymbium, Avicula nequivalvis, Pecten sublevis, and
P. dentatus, Belemnites, &e.

10. Table showing the range of the Fossils of the Rhetic Beds of
South Wales.

Southern- | Avicula-

Sutton series. down contorta
series. series.
{2 5
b as}

Species. S 4 : . ile

P e] | lel fl le zg

A S|) lac Sule. ae

“3 Sle Old ES

RD! & S)/Olb) .|S/ole dele

Stas Steels eles | Si fle

SISIS(SiS Si siti sisisisimica
M!OQ!)Olr = ao )a ao Miio| & .
SISSIES S/S/S/2 SiS Els lS
ei/Ss!10 w/|Sio Ret Rs) Pe
FIA BIA BAINIW Ola ly

22) US SILC AAS ee eee ieee Be BaP lites weal ere sia albert ies (e Se URL ovis

Pamela comtorta, OTE. 6. ...c0cecesetcleoalsac| cbaloos|eoe|aee Be aliamtcaatte alae ote Ae 9e [Le

Axinus elongatus, Moore .............. ale tel sie era | aoa eee oi sonfeeefs | % | 3
——— Mepressus, Moore .............2+20-[oee|se-fooelooefecsters FF cclieee ee venfooe| % | #
PO MCMAUIG, LOOTE: c.cos.ccn cs secede a|eaelecalvenleesdewaleee Laaleeeteeal ealets oe * | *

Myophoria postera, Qu. ..........eeeeefee Sellar alhisdeetto we sonia * [...| %
PeMierd Ma MOUNIIIA. 05... vdasaelnodeaesdeasee|eeslevefene a es eet eae % | % | K |
Anatina PULCHESOR QU. sac cdcee couse ds|easteas| ane baste ees rll isa lors % % | ¥
Memes Pylensis, Fawn. .........c0.cec|oee|oefooe Soe Seem et aes ae wefeo.] 2% | %

POMOnISICECUSSATA ~.........ccccerceneceloceloos DE IL en Nate celta laeade trinenlleatol te lose 3

PeESIVIAIGIMETISIS, POTEb le |. 2 S.scc0ess[ousloan|eqa[acafuceleasleesfasdloeelecclecs[ae| | ¥

* These beds were coloured as Rhetic by Mr. Bristow on the map of the
Geological Survey laid before the Bath Meeting of the British Association by
Sir R. I. Murchison in 1864. .

+ “ Buckland and Conybeare on the South-west district of England,” Trans.
Geol. Soc. 2nd series, vol. i. p. 294.

80 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 6,
Table (continued).
Southern-| Avicula-
Sutton Series. down contorta
series. series.
£ q
° S : * . Csi
Species. Se : F :
A elalFAl ieig IS
Sial |sisipl .jslale 310 |ro
“|RIEP TS /al/ei pe Bs ra gia ji
SiSidiSisiSisiSisislisisl ee
eee ree ets EISELE IBIS
EIS [alc Alas ASS le
Pleurophorus elongatus, Moore ......|...|..- soc esslece wi] Ssfe'orell oo a NIE
Ostrea liassica, Strick]. .........cceeecfeee]e Bhlstalconles ale sihecalllene * x
Plemaijpe dima; iS oe sais. <eakiesiseerost sides faee|e< ls a> aieis atsellereqol ie elelllntovallaretel leet ae % |... | 3
Acrodusacubuss Ages joc... .0.....ssnectee- sor|losalfoaolicdel|oas Spo b8ol locale acl su BP | al gee
eaNNaUbTA TIS, PAGE aaecoheaRDUROS One oooh BGe| holla] ado see[eeelece[eos(oee[eoe] % 1.00] 3
Saurichthys acuminatus, Ag. ......... wiasla'alnate lotta | cel ecg od halee cots ee shea | eae
SE PICBUIB AG. ii. seiniajone mnatiaonoe AACR Spe eiecc\AeAleorleslacclanelocoiiscaicca <> “5
Hybodus raricostatus, dg. ............/...}. éalicoe|idoclls apliacnisostess
ToEMaNO I AU/y ae bcdocasacs Lea senaeens coe[eaclees|ere[scoleceleos[eoe|-celae wale
—— phicatilis, dg. ............ si dice fe Ga etal | Mae ells al eal cite ers sees el oa
CUS Cats, AG. acest eaten a lectalere rallye loc eee yee sini [se tat oto
OLLMOCOMUSHAIZE?. see ete ee e sallasallestelleneloae iéel wae ROE
Gyrolepis tenuistriatus, Ag.............Jse{e.Jeos[...fe..]..- bs cleeehsccieee on eae
Aadlh Veith 4 1G/o) Bopoodoonae 5 visegeloevsctotel tase Wille ateectle ocoll se lowe of elo ES
Plicatula intusstriata, Hmm. ......... os oo *
acuminata, Ler. G7 Pleree see nec\een|ses| 7%
Ostrea multicostata, Miinst. ......... eee ee
levis, Tawn...... 5 Eades eel Del el eta ace % | %
Anomia socialis, Zawn. ..... Sard tial ges (etal asl ers te aan *
Pecten Suttonensis, Zawn. ........ wee | fo ee] 9 | a | 9 | 96 1% ]...] 4
ithericow Wowie npn sea. aces enleee Peal se ral geclene *
Lima tuberculata, Zerg. ...........-... He cote ose sine Spleso lone *
planicostata, Taw7................).+- % |e]...
angusta, Zawn. ....... Seifichaiick alee lpee *
subduplicata, Tawn. ............ spel cer Bee ene yl edna ae
Dunravenensis, Zawn. .........|...|..- * *
Pima insiemis, Wowie ws.4-co- ae! Relic alemeiate lie alse
Perna Ramsayi, Tawn. ......... Mtr Neal eel oe bdo Faniasellase *
Cardinia Suttonensis, Tawn. .........|...|... %
mgens, Monn. ralamatcesa aAstoosria|celladsl onn|izoulisac won|
Cardita rhomboidalis, Zawn. .........|...|...| %
Modiola imbricatoradiata, Tawn. ...}...|... *
Astarte Duncani, Zawn. ........... aah BA oe %
Cyprina normalis, Zawn....... sa re selec lial nea
Patella Suttonensis, Zawn. ............|..|...| #
Chemnitzia (NeW SPeCies)........ce0.0.-[oee|aee| % fenefe |
Turritella, sp. .....-. sjeiBore aterm anlar islet sate esl a *
Trochotoma, Sp. .........+ Bo tiat sacincs x
Ammonites Dunravenensis, Zawn....|. % | %
Ammonites Suttonensis, Zawn. ......]...|...].../...| *
Rhabdophyllia recondita, Lawbe......|...)...)...)... *
Thecosmilia rugosa, Lawbe.............{..+]. wallet es *
Hlyastrwa Fischeri, Laude. ........000[e0+|ecs|en-|oe- %
Astroceenia Oppeli, Laube. ............{...)..-]e.fe-- *
Moratla valley Spin Peper seapntarros cia 2 AMIE oe |iaellncek %

1865. | TAWNEY—RH TIC BEDS AND SUTTON STONE. 81

ll. Descriptions of the Spectes.

1. AmmontrtEs SUTTONENSIS, spec. nov.

I am unable to describe this Ammonite, the characters of the back
and keel not being sufficiently preserved in my specimens. Ina
side view it resembles A. Hettangiensis, Terquem, but it does not
seem to have a square and slightly keeled back like that species. It is
allied to A. Johnston or some of the ribbed “ Planorbes.” Diameter
1 imech.

* Locality and position—I have found this species about 20 ft.
above the base of the Sutton series, both at Dunraven and at the
Sutton quarries.

2. Ammonites DunRAVENENSIS, spec. nov. Pl. IV. fig. 1.

This fragment of an Ammonite differs entirely from the preceding,
being more involute, and it is more elongated.

Locality. Found 30 ft. above the base of the Sutton series at
Dunraven.

In form this species is allied to A. Hagenovi (Dunker), a shell
which, though from the Angulatus-zone, by the disposition of its
lobes and saddles is entirely allied to Ceratites (vide Terquem, “ In-
fralias de l’est de France,” in Mém. Soc. Géol. de France, 2nd series,
vol. vii. pl. x. figs. 3-5).

3. Prcten Etueripert, spec. noy. Pl. III. fig. 4.

Shell thin, suborbicular, equilateral, slightly convex. Surface
with numerous shallow or flat, not very closely set, radiating ribs, with
very fine concentric striz. ars large, unequal, concentrically and
radiatingly striated; anterior ear slightly hollowed out. Length
13 inch; breadth 3ths of length; umbonal angle 70°—75°.

Locality and position.—Sutton and Southerndown series at Sutton.

Affinities—This shell differs from P. calvus (Goldf.) in the ears
being less unequal and comparatively larger. It has much resem-
blance to P. Schneideri, Giebel, from the Muschelkalk, but is less
circular in form.

I have named this shell after my friend Mr. Etheridge, F.R.S.E.,
who has afforded me much help in the discrimination of the species.

4, Pucten Surronensis, spec. nov. PI. III. fig. 3.

Shell circular, convex, inequivalve, inequilateral. Left valve more
convex than the right; at the anterior side in both valves the ribs
bend forwards, producing the inequilateral form. Ribs alternately
larger and smaller; about twenty principal ones, between each pri-
mary rib a smaller, and between many of the secondaries occurs a
still smaller rib or carina. Ribs crossed by fine, concentric, raised
lines of growth, which curve downwards in crossing. In the
auricular regions, beyond the last rib, are broad lateral areas,
erossed by numerous, slightly wavy, oblique lines; posterior area
the wider; there is a steep fall from the areas by the last rib, down
to the ears, particularly in the more convex valve. Lars large,
unequal, posterior ear largest; in the right valve the anterior ear is

82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Deere,

hollowed out below; both ears have radiating coste and transverse
strie. Umbonal angle 110°-115°; length 22 inches ; breadth equals
length.

Locality and position.—Sutton and Southerndown series at Sutton.
Very abundant.

The exterior structure of the shell is frequently badly preserved ;
the concentric striations are then lost, and many of the smaller ribs,
but their alternate character remains generally more or less plain.

Affinities.—This shell is most nearly allied to P. Valoniensis (or
Lugdunensis, Michelin); it agrees with it and P. Bavaricus, Winkl.,
and P. Favrii*, Stopp. (all Rheetic species), in the characters of the
lateral areas, but with neither of them in the character of the ribs.
In general form and alternate arrangement of ribs it, resembles P.
Schreeteri, Giebel, from the Muschelkalk ; but that species has not the
obliquely marked areas. |

Some specimens of P. Valoniensis show a much greater resemblance
than others to this species.

5. PECTEN, sp.

Another orbicular Pecten I am unable to describe, having only one
imperfect specimen, the umbo being wanting. It is distinguished by
elevated strong concentric strie# in the interspaces between the ribs.
It has a slight resemblance to P. equivalvis ; but the ribs are more
numerous, narrower, and less regular than in that species; this shell
is also much smaller.

6. Lima TuBERCULATA, Terquem.

Shell moderately convex, suboval, slightly inequilateral. Ribs
11-12, narrow, radiating, bearing occasionally tubercles or remains
of spines; the ribs slope away gradually into the interspaces, which
are broad. Surface with concentric, more or less rugose lamine.
Posterior ear larger; anterior ear gaping below, somewhat plicated.
Hinge-line straight. Nolunule. Length 21 inches; breadth #ths
of length.

Locality and position.—Sutton and Southerndown series and Lias
at Bridgend.

This species is most nearly allied to L. onl ahonneas of the Inferior
Oolite, but is much smaller and less rugose. It corresponds entirely
with the description of Terquem’s species L. tuberculata (Mém. de la
Soe. Géol. de France, vol. vy. 2nd series, 1855). I have not hesitated,
therefore, to identify it with that species. It was described from the
Infralias (Planorbis- and Angulatus-beds) of Luxembourg, and
has been noticed by Renevier from the Rhetic beds of the Canton
de Vaud (Bull. de la Soc. Vaudoise des Sciences Nat. vol. viii.
p. 34); from the Infralias of the Department of Cote d’Or by
Martin (Mém. de la Soc. Geol. de France, 2nd series, vol. vi1.); and
I have also found it in the Planorbis-beds near Bridgend.

* This name seems preoccupied, having been given to another shell by M.
d’Archiac (1854) ; Stoppani’s name must therefore be cancelled, and I propose
to substitute for it the specific name of Renevierc.

1865. | TAWNEY—RH2ZTIC BEDS AND SUTTON STONE. 83

7. Lima PLANicosTaTA, spec. nov. PI, III. fig. 7.

Shell ovate, oblique, moderately convex, considerably longer than
broad. Surface of shell with distinct concentric lines of growth and
very faint radiating striz, which are most marked on the posterior
part of the shell. Kars unequal, the posterior largest. Length ?
to 14 inch; breadth 4ths of length.

Locality and position. —Sutton series at Laleston and Sutton &e.

This shell differs from LZ. precursor in form, and by the absence of
depressions in the interspaces between the ribs. It has some re-
semblance to LZ. compressa, Terquem, and to L. acuta, Stopp.; but the
sculpturing of those species renders them very distinct.

8. Lia aneusta, spec. nov. Pl. IIT. fig. 6.

Shell moderately convex, elongated, obliquely oval, inequilateral,
most arched in the centre. Anterior side straight for five-sixths of
its length and nearly parallel to the longer axis of the shell. Poste-
rior margin swollen in the centre and slightly concave below the ear.
Surface with regular, not very close or deep, radiating lines, eon-
centric striz, and lines of growth, which cross over the flat ribs. Au-
ricular areas sloping gradually into the umbo. Hinge-line straight.
No lunule. Length 23-3 inches; breadth 2ths of length.

Locality and ‘position. —Sutton series at Sutton and Dunraven.

My examples of this shell are rather weathered, so that the sur-
face-markings are not so well preserved as could be wished.

The form of this shell is characteristic. The shell that approaches
nearest to it is L. prelonga, Martin, from the Angulatus-zone of the
Department of Cote d’Or.

9. Lima suspurticata, spec. nov. Pl. III. fig. 8.

Shell ovate, slightly oblique, narrow at the hinge-line, convex.
Ribs about 25, elevated, not sharp; on the anterior and posterior
sides they become narrower and sharper, and the interspaces wider ;
interspaces with a fine costa between each of the ribs. Length 3 to
1 inch; breadth 2rds of length.

Locality and position.—Sutton and Southerndown series at Sutton
&c. Common.

The exterior of the shell is frequently lost, sel the cost are then
invisible.

Closely allied to L. duplicata (Great Oolite): it corresponds exactly
in form, but the line on the ribs is apparently absent. In its mature
state it is much smaller than L. pectinoides, neither are the ribs so
sharp, and the interspaces are broader than in that species. It resem-
bles an unnamed species figured by Quenstedt (Jura, p. 47, pl. iv.).

10. Liwa Dunravenensis, spec. nov. Pl. III. fig. 9.

Shell moderately convex, obliquely oval. Anterior side straight
for four-fifths of its length, and curving round. suddenly into the in-
ferior margin, which is strongly convex. Surface with numerous
fine, slightly wavy radiating lines, crossed by a few concentric lines
of growth. Length 34 inches; breadth 3ths of length.

84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 6,

Locality and Position.—Sutton and Southerndown series at Dun-
raven &c. Common.

From the imperfect state of my specimens, I am unable to say
whether the interspaces between the ribs are punctated.

This shell is distinguished from Z. punctata by its straight ante-
rior side; the size of the ribs brings it nearest in character to
Inma Valomensis, Def., cited by Dumortier (Dépéts Jurassiques du
Bassin du Rhone, p. 54) as occurring associated with Pecten Valo-
neensis, Def. In form it bears much resemblance to L. ewaltata,
Terquem, from the Infralias of the province of Luxembourg; but
the ribs are a little wider than in that species. In the absence,
therefore, of the characters of the whole shell I cannot identify it
with either of these species.

11. Lr, sp.

I have the hinge-area of a remarkable Lima which bears a great
resemblance to the hinge of Zama cometes, Dumortier, ‘ Bassin du
Rhone,’ pl. xxii. figs. 1 and 2; butin the absence of the rib-charac-
ters I cannot identify it, as by its form it is also allied to Z. tuber-
culosa (Terquem). The hinge-line is not straight, but forms an
obtuse angle with the ears; the ears are strongly plicated. No lunule.
The shell is very thick around the ligamental pit, but is abruptly
hollowed out below.

12. OstrEa Levis, spec. nov. Pl. III. fig. 2.

Shell extremely convex, elongate, and ovate. Surface with con-
centric, somewhat irregular, fine, imbricated folds of growth or deli-
cate wavy lamelle. Margin thick and entire. Length 14 inch;
breadth 2rds of length.

Locality and position.—Sutton series at Sutton and Langan. Com-
mon.

This shell varies in different localities, being sometimes very nar-
row ; it is readily distinguished from Ost. liassica by its convexity,
and does not occur in such numbers together as that species.

13. OstrEa munticostata, Minst. Pl. III. fig. 1.

Shell elliptical, frequently nearly equilateral, thick. Umbo near
the hinge, from which strongly elevated straight or slightly wavy
ribs‘diverge; ribs acutely rounded, crossed by fine concentric lines
of growth, equally visible in the interspaces ; interspaces the same
size as the ribs. Ribs extend to the margin, causing it to be undu-
lated; margin thick, rounded. Length 3 inches; breadth $ths of
length.

Locality and position.—Sutton and Southerndown series at Sutton
&c. Common and characteristic species.

The area of attachment is devoid of ribs and frequently occupies a
large portion of the shell.

This shell is variable, affecting at different times the appearance
of O. spondyloides, O. multicostata, and O. difformis. Terquem, in de-
scribing the Ostree of the Province of Luxembourg, proposed to unite ~

1865. ] TAWNEY—RHZETIC BEDS AND SULTON STONE. 85

‘these three Muschelkalk species, as there is little apparent differ-
ence between them; but subsequently (“‘ Infralias de lest de France,”
in Mém. Soc. Géol. de France, 2nd series; vol. viii.) he deemed it un-
advisable to refer his species to them or the genus Ostrea, and it stands
as Carpenteria Heberti. As the Sutton fossil bears considerable resem-
blance to Terquem’s figures, it is with much diffidence that I con-
tinue to refer it to the Muschelkalk type ; the examination, however,
of several specimens having the same character of the umbonal region
leaves no doubt in my mind of its being an Ostrea; and the descrip-
tion of O. multicostata corresponds entirely with our shell.

In some of my specimens the ribs are not so elevated and regular,
but more lamellar; but these differences may be ascribed, I think, to
a young state; others show a likeness in external characters to Pli-
catula Baylii (Terquem), but as I have not seen the hinge, I must
leave it to future researches to settle this point.

Affinities.—This shell bears some resemblance to Ostrea arietis of
the Angulutus- and Bucklandi-beds), but is still more nearly allied
to O. Rhodani, Dumortier, from his Planorbis-zone *. He figures also
a fragment, which may be allied to this species, as passing up into the
Angulatus-zone ; he considers it to be allied to the Muschelkalk spe-
cies, Ostrea complicata (Dumortier, Bass. du Rhone, pl. xxiii. fig. 6).

14, Anomra soctatis, spec. nov. Pl. III. fig. 10.

Provisionally I call this shell Anomia, from its shell-structure; there
are not, however, in.my possession data enough to safely determine
or describe the specific characters. Its abundance, however, in some
localities where it occurs in groups, renders it a most noticeable
shell; I therefore name it as above. Length 14 inch.

Locality and position.—Sutton series at St. Mary Hill. Common.

This shell has a great resemblance to Ostrea subanomia (Miinst.)
from the Muschelkalk, but I cannot with any surety refer it to that
species.

15. Pinna Insre@nis, spec. nov. Pl. III. fig. 5.

Shell thin, acute at the umbo, broadly wedge-shaped ; posterior
extremity gaping, strongly rounded, and truncated. Dorsal edge
thickened and well defined. Surface smooth, with broad, wavy, con-
centric folds. Length 7 to 8 inches; breadth 4 to 5 inches.

Position and locality.—Sutton and Southerndown series at Sutton
and Dunraven.

This shell is most usually found in quite a fragmentary condition ;
it attained a large size, and was a widely gaping form.

Notwithstanding the imperfect state of my examples, I am obliged
to create a new species. It differs considerably from Pinna semi-
striata, Terquem (Pal. de Lux. pl. xxii. fig. 1), being, comparatively
wider, and the concentric folds do not show the same disposition.
It is also more pyramidal than Pinna papyracea, Stopp. ., and the
shell is not so extremely thin as in that species.

* Dumortier includes in the Planorbis-zone- beds containing Pecten Valoniensis
aa Plicatula intusstriata abundantly.
VOL, XXII,—PART I, H

86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 6,

16. Perna? Ramsayi, spec. nov.

Shell oblique, elongated, moderately convex, thin. Surface with
rounded wavy concentric folds, which extend across the shell. Ear
large, crossed by see folds or lines. Hingeunknown. Length
4 inches ; breadth $ths of length. ;

Locality and ei: —Southerndown series near Sutton.

My specimen only shows the interior of the shell, which is, how-
ever, very thin. The hinge-line also is broken off, so that the genus
is uncertain. It bears some slight resemblance to Perna infraliasina
Quenst., but it is considerably larger than that shell. Until the ex-
ternal shell is known, it cannot be referred to that species. I dedi-
cate it, therefore, provisionally, to Prof. A. C. Ramsay, F.R.S8., Pro-
fessor of Geology at the Royal School of Mines.

17, PxicatuLa acuminata, Terq. et Piette.

I have specimens corresponding to the description given of this
shell by Terquem and Piette (Mém. Soc. Géol. de France, 2nd series,
vol. vil. p. 107, pl. xii. figs. 20, 21), the distinguishing character
being the acute hinge with transverse folds and radiating ribs. They
cite it as a rare shell, in beds containing Belemnites acutus.

18, PLiIcaTULA INTUSSTRIATA, Emm. °

This is one of the most characteristic species. In England it is
a characteristic Rheetic species ; but on the continent it passes up into
the Planorbis-zone, if not higher. The species P. Lotharingie, Terq.
et Piette, evidently belongs to Emmerich’s type; it is cited from
the Planorbis-zone. Dumortier says (Infralias, p. 76) that it is
characteristic of the Planorbis-zone, never being found below or
above; it is probable, therefore, that his Planorbis-zone corresponds
to the upper part of our Rheetic series, including the White Lias.

19. Carpinia Surronensis, spec. nov.. Pl. IV. fig. 3.

- Shell transversely oblong, obovate ; ventral margin gently rounded ;
anterior end broadest, obtuse; posterior end subacutely rounded.
Surface with deep, concentric, distant lines of growth, and smaller,
elevated, intervening striz, which become less distinct at the posterior
end. Umbones somewhat acute, placed about one-fourth of the length
from the anterior end. Length 21 inches; breadth 2rds of length.

Locality and position. Sutton quarries, "Sutton series.

This shell is nearest in form to C. regularis, Terquem; but the
posterior end is more acute than in that species; the size is also
larger, and the shell thicker. It is less cuneiform than C. acuminata,
Martin, to which it bears some resemblance.

20. CaRDINIA INGENS, spec. nov. Pl. IV. fig. 2.

This large cast of the interior is from the Sutton series near
Langan. My specimens do not show the outside of the shell. All
that I saw with the outside shell were in an earthy condition and

1865.] = + TAWNEY—RHZETIC BEDS AND SUTTON STONE, 87

crumbled on being moved. ‘The concentric folds of growth were
distinct and strong.

It approaches nearest to C. crassissima, Ag.; but the pallial line
does not quite agree with that species.

21. Carpita? RHOMBOIDALIS, spec. noy. PI. IV. fig. 6.

Shell convex, rhomboidal ; a rounded ridge extends from the
umbo to the posterior margin. Dorsal and ventral margins nearly
parallel; posterior end of shell widest. Umbones placed far for-
wards, somewhat recurved. MHinge-line straighv. Interior margin
of the shell delicately crenate. Surface with regular, elevated, con-
centric lines, which cross over the rounded ridge, and, by a sharp curve,
reach the dorsal margin. Length 1 inch; breadth 2rds of length.

Locality and position.—Sutton quarries, Sutton series. Common
near the base.

The shell-substance is rarely found. The mould of the inside
drops out of the cast, leaving the impression of the exterior surface:
from this gutta-percha casts may easily be obtained.

Not having seen the hinge-teeth, I am uncertain of the genus.

It somewhat resembles Cardita tetragona, Terquem ; I therefore
refer it provisionally to that genus. -

-22. MopImoLa IMBRICATO-RADIATA, spec. noy. Pl. IY. fig. 8.

Shell small, convex, transversely oblong, comparatively thick. A
rounded elevated dorsal ridge extends from the umbo to the posterior
margin. Posterior margin rounded ; ventral slightly concave. Sur-
face of shell ornamented with numerous radiating rounded ribs, which
are slightly wavy and sometimes forked, crossed by a few growth-
lamelle.. Umbones obtuse, placed far forwards. Length 0-6 inch ;
breadth 2rds of length.

Locality and position.—Sutton quarries, Sutton series. Common
near the base.

The ornamentation is like that of the Oolitic species M. pul-
cherrima ; it reminds us also of Mytilus furcatus, but is very much
smaller, the margin not so concave, &e. :

23. Asrarte Duncant, spec. nov. PI. IV. fig. 4,

Shell convex, rhomboidal, inequilateral, widest at the posterior
end; posterior margin rounded and forming rather less than a right
angle with the ventral margin. Surface of shell with strong con-
centric lines of growth wider apart posteriorly, and intervening finer
_ones. Umbones placed far forwards. Length 3inch ; breadth ths

of length. cules
Locality and position Sutton quarries, Sutton series.
The genus of this shell is not quite certain, my specimen, not
showing the hinge-line.
It is named after our Secretary, who has kindly undertaken the
description of the corals from the Sutton Stone.

24, CYPRINA NORMALIS, spec. nov. Pl. IV. fie. 7.
Shell suborbicular, convex, inequilateral, thick, Umbones slightly
H 2

88 PROCEEDINGS OF THE GEOLOGICAL society. — [ Dec. 6,

anterior, acute. Surface concentrically marked by numerous lines of
growth. Anterior side well rounded; posterior subacute. Length
8 to 1Linch; breadth #ths of length.

Locality and position, ”—Sutton quarries, Sutton series.

The form of this shell renders it probable that it is a Cyprina. I
have not seen the hinge, owing to the unfavourable state of the
matrix.

25. ANATINA PR=CURSOR, Quenst., var. Pytensis. Pl. IV. fig. 5.

Shell flatly convex, transverse, inequilateral. Anterior end
rounded ; posterior end slightly produced, narrower, and somewhat
depr essed. Lines of growth consisting of from six to ten concentric
rounded folds, which extend along the shell, being nearly as distinct
posteriorly as anteriorly. A slicht ridge proceeds from the umbo to
the postero-ventral margin. Ventral margin rounded. Umbones sub-
central, depressed posteriorly. Length "1h inch ;_ breadth half of
length.

Locality and position.— Avicula-contorta sandstones at Pyle, Stormy
Down, &e.

This shell differs from the description given by Oppel and Suess in
being considerably shorter posteriorly. It approaches thus more to
the form of A. Suessit, but it lacks the median depression which hol-
lows out the ventral margin of that species. It differs from Oppel’s
figure of A. precursor by the extension of the folds along the posterior
part of the shell as they curve round to meet the dorsal margin.

These differences are perhaps enough to constitute a new variety,
but do not, I believe, necessitate the formation of a new species.

26. PaTELLA SUTTONENSIS, spec. nov. Pl. IV. figs. Da, 9 6.

Shell convex, oval. Apex not quite central, but nearest the pos-
terior margin, and the highest point of the shell. Surface covered
with regular, elevated, slightly imbricated, concentric lines, which
become a little fainter near the apex. Length ?inch; breadth ?ths
of length.

Locality and position.—Sutton quarries, Sutton series.

This shell has much the aspect of a Discina; but as it is not horny
in texture (neither have I found a lower valve), I refer it to this
genus.

It resembles Patella elliptica, from the Muschelkalk, and also
P. Hettangiensis, from the Angulatus-beds of Hettange ; it clearly
differs, however, from these species. The form differs from P, Het-
tangvensis in the region of the apex especially.

27. CHEMNITZIA, sp.

There is a large univalve shell, 43 inches long, common in a bed
near the middle of the Southerndown series ; natural sections of the
shell, showing the columella, may sometimes be seen on the beds,
which have been slightly polished by the sea. I have nospecimens,
owing to the difficulty of breaking up the beds at this place,

1865. ] DUNCAN—SUTTON-STONE CORALS. 89

28. TURRITELLA, Sp.

I have some small species from the Sutton Stone which may belong
to this genus and to Chemnitzia, but which it is impossible to recognize
specifically.

29. TrocHoToMA, sp.

A very flat form from the Sutton Stone may probably be referred
to this genus. Its imperfect state prevents a description.

30. Natica Pytxnsis, spec. noy. PI. LY. fig. 10.

Shell ovate. Body-whorl large. Spire depressed, of two volu-.
tions. Suture deeply impressed. Apex blunt. Aperture semicir-
cular. Length 0-1 to 0°3 inch.

Locality and position.—Avicula-contorta sandstones at Pyle and
Stormy Down.

This shell never exceeds the above small dimensions ; it generally
occurs in the form of casts. It is both gregarious in great numbers,
and occurs singly.

Note on the Mavruporarta from the “Surron Stone.”
By P. Martin Donean, M.B. Lond., Sec. G.S.

Tn collection of Madreporaria from the base of the Sutton Stone con-
tains a considerable number of specimens, some of which are de-
rived fossils, and the others, generally in a very fair state of preser-
vation, indicate a lower coralliferous horizon than has been hitherto
noticed in the British Secondary rocks.

A fine-grained white limestone with much cale-spar is the matrix
of the Secondary corals; and the Paleozoic are contained in a rougher
stone, more or less conglomeratic. The neighbourhood of the Car-
boniferous Limestone accounts for the presence of its fossils at the
base of the Sutton Stone; and the derived species therein contained
are well known and char acteristic.

The species are :—

1. Lithostrotion irregulare. | 2. Amplexus coralloides.°

These forms do not require any notice; they are unlike any from
Mesozoic sources, and are very common in the Carboniferous strata.
The specimens of the fine-grained limestone which contain undoubted
Secondary corals are numerous, and the fossils are either well pre-
served or are in the form of casts.

Four species can be determined satisfactorily, or rather three
species and three varieties of a fourth, whose Alpine type is not pre-
sent. The subgenus of one other form can be recognized ; and in all
probability the numerous casts must be referred to it. The species
are unlike any hitherto discovered in North-western Europe, and,
with certain reservations, indicate a zone of Madreporaria which in
the Alpine Trias would. be deemed St. Cassian.

The great ‘Monograph of the British Fossil Corals,’ by MM.
Edwards and Haime, does not contain a description of any species

90: PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 6,°

from the Lower Lias, and there still remains a great gap in our know-:
ledge of the Madreporaria, between the Permian and the Liassic strata
yielding Jsastrea Murchisoni, Wright, and Lhecocyathus Moorer,
Ed. & H.

Lately, large series of Middle and Lower Liassic corals have passed
through my hands, and MM. Chapuis and Dewalque in Belgium, De
Fromentel in France, and Stoppani im Italy have described species
which have enabled me to mark out the characteristic species in our
Middle and Lower Lias. The species from the Sutton Stone have
nothing in common. with any species from the Liassic strata.

The White Lias of Somerset has yielded two species of Corals*.
Unfortunately the condition of these fossils prevents their specific
determination ; but they belong to the genus Monthvaltia. One is a
broad flat form, and is probably allied to the Montlivaltie of the
Lower Lias, which are usually more or less discoid. The other spe-
cimen is a small tall and conical form, with well-marked transverse
ridges on its epitheca. This peculiarity i is to a certain extent Liassic ;
but the stunted growth and the apparently multiseptate arrange-
ment ally the form to the Triassic Montlvaltie. Neither of the
White-Lias forms are contained in the collection from the base of the
Sutton Stone. A Monthvaltia was discovered in the Avicula-contorta
series at Beer Crowcombe, by Mr. Chas. Mooret.

In the late researches of Reuss upon the Madreporaria of the
Kossen strata, numerous species were determined ; some ascend into
the Lias, according to Stoppani; and all have a good Secondary facies,
there being no traces of Paleozoic genera.

The corals of the Dachstein series are still in a very unsatisfactory

state, as regards their description; but it will suffice to assert that
they are not of the Paleozoic genera Lithodendron and Cyathophyl-
lum; on the contrary, the species belong to the genera which domi-
nated during the Jurassic epoch.
. It is. now tolerably evident that all the St. Cassian corals formerly
associated with Paleozoic generic names are Mesozoic forms, and
that only two new species, carefully determined by Reuss, belong
to aS many genera, one being Paleozoic, and the other closely allied
to a Paleozoic genus.

- Recently Gustav Laube + has concluded the examination of
Aiki re and Klipstein’s St. Cassian Sponges, Corals, Crinoids, and
Echinoderms: he has not distinguished a single Paleozoic genus
amongst the Corals, but he has determined the great distinction be-
tween the Liassic and Triassic coral faune.

It is the defective information respecting the corals of the Dachstein
series, and of the relation of the St. Cassian corals to those of the
Dachstein and of the Kossen strata, which causes me to make a re-
servation in my opinion about the age of the Sutton-Stone species. In
other words, there is insufficient information concerning the vertical
range of the St. Cassian species of Corals ; and the discovery of some of

* Boyd Dawkins, Quart. Journ. Geol. Soc. vol. xx. P. 406.

tT Quart. Journ. Geol. Soe. vol. xvii. p. 511.
ti ‘Die Faune der Schichten von St. Cassian, 1 Abtheil.

1865.] | . DUNCAN——SUTTON-STONE CORALS. 91

them in South Wales adds to the probability of their haying a greater
vertical range than has hitherto been supposed, from their fol-
lowing the law that the widely wandering 1 in space are persistent in
time. ©

There are some considerations respecting the range of | some Rheetic
and Liassic mollusca, both in England, France, and Switerland, and
concerning the alternations of the Piece contorta and Dachstein-
bivalve and the coralliferous strata in the Késsen and Dachstein di-
visions of the Alpine Trias, which strengthen the necessity for caution
in correlating distant Triassic strata possessing species In common.

Moreover it cannot be admitted that the coral fauna of the period
is fairly represented in the Alpine Trias, great as its number of
genera may be. It is also remarkable that the Avicula-contorta
series should be very uncoralliferous: doubtless the Avicule with
their associated bivalves and generally puny Gasteropods were
dwellers in a muddy area, where only stunted and simple Madrepo-
raria can live.

The alternations of the strata just mentioned, and the great vertical
range of some species, indicate that although the succession of the
Upper Triassic, Rheetic, and Lower Liassic strata is to be traced in
ascending order, still this succession may have a very doubtful chro-
nological meaning. The species which form the little coral fauna of
the Sutton series do not indicate a vigorous condition of the polype-
life of the period: their affinity with the Alpine St. Cassian species
is beyond doubt; and whatever their age may be, they are still the
oldest amongst: the Mesozoic forms in this country.

This is a conclusion which was determined irrespectively of Mr.
Tawney’s researches, and it is strengthened by them. The absence
of the usual species of the mollusca of the Avicula-contorta beds, the
close proximity of these beds, the existence of a number of local spe-
cies, and the localization of the Sutton Stone in the west indicate
that the series resting on the Mountain-limestone is older than the
“< contorta”’ -bearing strata. How much older, is of course subject to
the application of the remarks already made.

Inst of the Species.

1. Rhabdophyllia recondita, Laube. | 4. Astroccenia Oppeli, Laude, 3 vars.

2. Thecosmilia rugosa, Lawbe. 5. Montlivaltia, sp.

3. Elyastrea Fischeri, Laube.

Remarks on the species.—The three species at the head of the list
are described and admirably delineated in Gustav Laube’swork. Rhab-
dophylha is a well-known Jurassic genus, and was doubtless one of
those misnamed Zithodendron in the Alpine Trias. The species recon-
dita is a very well-marked one, and the singular disposition of the
smaller septa to bend towards the larger is very distinctive. The
genus is unknown in the British Lias, and the species is only re-
motely related to the Oolitic forms.

The Thecosmilia rugosa 1s a compound coral, stunted in growth,
and given to fissiparous division of its calices; the rugose transverse
markings of the epitheca are well shown, both in Laube’s drawing

92 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 6,

and in the Sutton species. So alike are the drawing and the
specimen that it might be asserted the one was taken from the
other.

The genus Elyastrea described by Laube is new, and not known
out of the St. Cassian strata; itis allied to the Mesozoic genera He-
liastrea, Isastrea, and Prionastrea, and it has some faint trace of the
double-wall arrangement of many Paleozoic genera. Heliastrea and
Prionastrea flourished in the Oolitic and Cretaceous periods, and are
still represented in the existing coral fauna, but Jsastrwa was a St.
Cassian genus, and lasted until the Falunian epoch. The discovery of
the genus which unites all these sufficiently to make their generic
distinction doubtful, is very important, and that it should occur so
low in the Mesozoic series is very suggestive. The species Fischerz
is a bulky form, with very irregular calices, and is represented in
the Sutton Stone by a large specimen partly polished.

The most common coral in the collection is one which has a broad
base and an undulating gibbous surface, covered with small geo-
metrical calices. This is the commonest form ; but another is equally
large as regards its base, and has a flat upper surface covered with
calices, like the gibbous form. There is not a specific difference.

A third form covers, like a parasite, part of the surface of
the Rhabdophyllia recondita; the calices are smaller than in the
other forms; but they are all essentially alike. It is remarkable
that the Rhabdophyllia in its St. Cassian habitat is covered by a
parasitic sponge.

The three varieties of Astrocenia Oppeli are judged to be such
because the minute anatomy of the calices is alike in all cases, and
that the habit of growth of the type is not sufficient to enable it to
assume a specific difference. It is a pity that Laube had not the
larger Sutton variety for the type; but he has the right to have the
three forms referred to his by priority of description. I have named
the varieties—

1. Gibbosa, | 2, Plana,
3. Parasitica.

The genus is well known in the Lower Cretaceous, Kocene, and
Miocene coral faunz, but has not been found hitherto in Jurassic
deposits. “4s

The Montlivaltia from the Sutton Stone is a stunted, multiseptate
form, with a ridged epitheca; it resembles the general type of that
section of the genus which is almost peculiar to the St. Cassian
coral fauna. The casts of it are common, but the specific deter-
mination is impossible.

EXPLANATION OF PLATES III. & IV.
Illustrative of the Rhetic Fossils of South Wales,
Puate ITI,

Fig. 1. Ostrea multicostata, Minst. Sutton and Southerndown series.
levis, Tawn. Sutton series.

CRB pee . del. eb lith , ; 7 M & i Eee ees imp:

AHATIC FOSSILS FROM SOUTH WALES |

*}
‘ y f t
»
i
\ '
N ht te
a
<t
i
i al
i LM i 9) 7 ‘ *
f al " bey den
i) f A a
j
Loe ai)
K /
¥ *
'
a hy
” - .
=)
‘
bo 4
fi
‘
a
‘ t
‘

iter deme col Soc Nol xk alig = lays

a Prien del et lith. . Mé&NHanhart imo
‘ Pe ie Ee sst Ss FROM SOUTH WALES.

1365. | BRODIE—LOWER LIAS AND RHATIC BEDS. 93

Fig. 3. Pecten Suttonensis, Tawn. Sutton and Southerndown series.
EKtheridgit, Tawn. Sutton and Southerndown series.

. Pinna insignis, Tawn. Sutton and Southerndown series.

. Lima angusta, Tawn. Sutton series.

—— planicostata, Tawn. Sutton series.

subduplicata, Tawn. Sutton and Southerndown series.
—— Dunravenensis, Tawn. Sutton and Southerndown series.
. Anomia socialis, Tawn. Sutton series.

Puate IV.

Fig. 1. Ammonites Dunravenensis, Tawn. Sutton series.
. Cardinia ingens, Tawn. Sutton series.
. —— Suttonensis, Tawn. Sutton series.
. Astarte Duncani, Tawn. Sutton series.
. Anatina precursor, Quenst. Avicula-contorta sandstones.
. Cardita rhomboidalis, Tawn. Sutton series.
. Cyprina normalis, Tawn. Sutton series.
. Modiola imbricato-radiata, Tawn. Sutton series.
9a, 96. Patella Suttonensis, Tawn. Sutton series.
10. Natica Pylensis, Tawn. Avicula-contorta sandstones.

DD ODT OS

eel

MTS Ot} Oo bo

2. Notes on a Suction of Lowrr Liss and Ruztic Buns, near WELLS,
Somerset. By the Rev. P. B. Bropim, M.A., F.G.S.

Tue accidental lowering of a road at Milton Lane, one mile anda
half north of Wells, exposed a very interesting section of Lias and
Rheetic beds, which has not been referred to by Mr. Dawkins in his
paper ‘‘ On the Relations of the Liassic and Rheetic Series in Somer-
setshire.”’ This section is the more deserving of notice because, as
a general rule, the sections in the immediate neighbourhood only
exhibit the White Lias and Rheetic beds, and these have not hitherto
been recorded so near the city in a northerly direction, nor so close
to the Mendips; and in this case we have the “‘ Lima-beds” the highest
seen, passing into and overlying the White Lias and the Avicula-con-
torta zone. ‘The nearest section to Wells described by Mr. Dawkins,
showing the White Lias and Rheetic series, though very obscure, is
at Pen Knowle, about five miles west of the town. The Milton-Lane
section gives a clearer view of the succession of the “ Lima-beds”
downwards, and I can confirm Mr. Dawkins’s* statement that the
«White Lias” rests immediately upon the Rheetic bedst ; for whether
the strata below No. 4 in the annexed section, down to the “ White
Lias,” belong to the ‘‘ Lima series,” which is most probable, and to
“which if have referred them, or form a reduced equivalent of the
"s Insect and Saurian beds,” it is evident that the latter do not here or
‘elsewhere underlie the “ White Lias.” The following is the sectiont
at Milton Lane, in descending order :—

* This was also pointed out by Mr. Bristow in his paper communicated to the
Bath Meeting of the British Association.

t+ At Harbury, in Warwickshire, the Lima-beds rest immediately on tke
White Lias.

{ This section was taken conjointly with my friend Mr. James Parker.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 6,

ive)
=

Section at Milton Lane.

. Thick blue limestones, compact, containing Lima gigantea, feet. inches.

L. duplicata and another species, Hemicardium cardio-

ides, Pinna, Myacites, Pecten, Pholadomya, and Wald-

heimia perforata (same species as in No. 4), Ammonites

Bucklandi, A. Conybeari, and Nautilus striatus ......... 5
. Clay and bands of indurated rubbly limestone, often no-

dular, with many fossils, especially Lima gigantea ...... G. @
. Thicker beds of sandy limestone, divided by sand, from

4 to 8 inches thick ; very fossiliferous ..............ssese« 4 0
. Sandy limestones and intercalated shale, numerous fos-

sils—Lima duplicata, Iima?, small Avicula, Trochus

(same species as in No. 5), and Waldheimia perforata* '7 0
. Hard sandy shelly limestone, very fossiliferous, with par-

ticles of quartz, and shaly partings 2 or 3 inches each,

yielding Ammonites (very imperfect) and casts of As-

tarte and Trochus...... si gauisefagaa waste Cet scan cake ak uaee eee a met
. White Lias limestone, hard, close-grained, containing the

usual fossils, especially Cardiwm Rheticum, Modiola

Hillana, Lima, and Pecten. I did. not observe Ostrea

THUUSSUTUALG, MOY BUY COVAIS . 121-25: --eeee ore eee eee 0 eee
. Soft marly shale (base of White Lias), with Modiola mi-

nima, M. Hillana, Cardium Rheticum, Lima, and

Spiny PUICO LUG. occiccent Jens aban sncbncee een eee eee eee) nearer 3 0
. A peculiar bed, with much quartz, broken and rubbly ... 1 6
. Black shales, with thin layers of selenite in some parts,

and frequent traces of peroxide of iron, from 6 inches

to 3 inch thick. Contains Cardiwm Rheticum and Avi-

cula contorta unusually well preserved, and casts of other

small bivalves and apparently some minute seed-vessels

+t

LS)

“~
H Co

Lima-beds.

Cr

lor)

White Lias
—_- ~. ———$—$$__*~—___—._ __—— SS
co 00 “I

8 of some plant. The shells were tolerably abundant, but
a the Seneta LOW, oa: sosseace- Mccicadereaesgeses-eseee. gee eres 8 0
2 410. Grey marl ; with the exception of traces of small plants, .
= | ne fossils were observed «...21itirseszessacth- sass scegoeeeeenae 2 6
8 11. Alternations of clay and marl, rather variable, about 3 or
& 4 inches Lhjele ss. Wsiies duds acdaser odasee fo cssec anaes n eee 2 6
12. Hard grey marl, similar to No. 15, becoming harder as it
ASCEMGS. vy «x>s ceegst ons gocanr tame tars een e Meeaenee see eee eee 2 6
13. Soft green maritand shales ticccccse--aror trea ote. nee Sieaeee ye 3 ae
14. Series of grey and yellow marls, with layers of marl near
=e the top, where it 1s more indurated! .....- 200 -n.n-careute ee
way (ly., Mila ly ayachlag er eats eee oes canner eee slat wis’ sucoe ener 8 tie
ey | 16. Red and white marls.

The Lima-series here amounts to 27 feet, the White Lias to 10
feet 4 inches. The Rhetic (including the grey marls) to 18 feet 6
inches. I could see no trace of Ammonites planorbis, nor any of the
peculiar limestones indicating the “ Insect and Saurian” zones, which
seem to be entirely wanting, the Lima-beds resting immediately
upon the “ White Lias.” There is certainly a greater thickness of
Lias at this spot than might have been at first sight expected, con-,
sidering that, as a whole, it thins out towards the Mendips, with,
which it here comes into almost immediate contact. The direction
of the lane is nearly at right angles to the strike of the beds, which
dip about ten degrees, but somewhat irregularly, being much dis-
turbed to the north-east. I found one piece of bone-bed lying loose
at the lower end of the lane, near the bed No. 14, full of bones, teeth,

* Most of the shells in nos, 1 & 4 were too imperfect for determination of the
species.

1865. | DAWSON—COAL-FORMATION. 95
and scales of fish (Hybodus), &c. ; but after a careful search on several
occasions, neither Mr. Parker, myself, nor the workmen could find
any more, or discover its exact position im situ. The lithological
character of this ‘“‘ bone-bed’’ was rather different from that which it
usually presents, the bones and teeth being imbedded in a hard mass
of limestone-conglomerate, made up of lighter. coloured angular frag-
ments of limestone forming a kind of coarse breccia. On another
visit to Milton Lane, after I had left Wells, Mr. Parker informed
me that a further excavation nearer to the Mendips exhibited a
slight difference in the stratum No. 8, which was much faulted and
broken up, one side being let down, with an intervening band of dark
shale belonging, I suppose, to the “ Avicula-contorta zone.”

DecemBer 20, 1865.

_ Hugh Leonard, Esq., C.E., Calcutta ; William Lyon, Esq., J.P.,

Wellington, New Zealand; Moses Pullen, Esq., Painswick, Glou-

cestershire; and Charles Stavely Rooke, M.1.C.E., 12 Blenham

Terrace, Leeds, were elected fellows.

The following communication was read :—

On the Convitions of the Derosition of Coan, more especially as
illustrated by the Coat-rormation of Nova Scorra and NEw
Brunswick. By J. W. Dawson, LL.D., F.R. os F.G.S., Principal
of M°Gill (ilies: Montreal.

[Puates V—XIT.]
ConTENTS.

I. Introduction.
II. General Considerations relating

Plants whose remains occur in
the Coal.

to Physical Conditions. 1. Introduction.
1. Physical Characters of the several 2. Coniferous Trees.
Coal-formations. 3. Sigillarie.
a. The Upper Coal-formation. 4. Calamodendron.
6. The Middle Coal-formation, 5. Calamites.
or Coal-measures proper. 6. Asterophyllites, &c.
ce. The “ Millstone-grit” for— 7. Filices.
mation. 8. Megaphyton.
d. The Lower Carboniferous 9. Lepidodendron.
Marine formation. 10. Lepidophloios.
e. The Lower Coal-measures. 11. Cordaites, or Pychnophyllum.
2. Physical Conditions attending 12. Sporangites.
the Deposition of the Coal- 13. Tissuesin the Mineral Charcoal.
formations. a. Bast tissue.
3. Geological Cycles. 6. Vascular bundles of Ferns.
4. Summary of facts relating to the ec. Scalariform vessels.
- mode of accumulation of Coal. d. Discigerous wood-cells.
III. Details of the Character and Fossil e. Epidermal tissue.
Contents of the several Beds of 14. Rate of growth of Carbonife-
Coal, as exposed in the South - rous Plants.
. Joggins Section. 15. Bivalve Shells.
1, Introduction. 16. Spirorbis carbonarius.
2. Logan’s Section. 17. Crustacea.
a. Division 1. e. Division 5. 18. Fishes.
6. Division 2. f. Division 6. 19. Land-animals.
ec. Division 3. g. Division 7. | V. Appendix: Descriptive List of

d. Division 4. h. Division 8.
IV. Remarks on the Animals and

Carboniferous Plants found in
Nova Scotia and New Brunswick.

96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

§ I. Inrropvction.

In several former papers presented to this Society, I have endea-
voured to illustrate the arrangement of the Carboniferous rocks of
Nova Scotia, and to direct attention to their organic remains, the
structures found in their coals, and the evidence which they afford
as to the mode of accumulation of that mineral. The present paper
is intended as the summing up and completion of these researches,
with the addition of the new facts resulting from a careful study of
the microscopic structure of more than seventy beds of coal occurring
in the South-Joggins section, and of the fossil plants associated with
them. These results will, I hope, throw much additional light
on some of the more difficult problems connected with the theory of
the accumulation of vegetable matter in the Carboniferous period,
and its conversion’ into coal.

The subjects to which I propose to direct attention may be con-
veniently arranged under the following heads :—

(1) General considerations relating to the physical conditions of
the Carboniferous period in Nova Scotia.

(2) Details of the character and contents of the several beds of
coal in the Joggins section, arranged in the order of Logan’s
Sectional List. ,

(3) Remarks on the genera of animals and plants whose remains
occur in the coal, and on their connexion with its accumulation,

§ IT. Generar ConstDERATIONS RELATING TO PHystcaL Conpirrons.

1. Physical Characters of the several Coal-formations.—The total
vertical thickness of the immense mass of sediment constituting the
Carboniferous system in Nova Scotia may be estimated from the
fact that Sir W. E. Logan has ascertained by actual measurement at
the Joggins a thickness of 14,570 feet; and this does not include
the lowest member of the series, which, if developed and exposed in
that locality, would raise the aggregate to at least 16,000 feet. It
is certain, however, that the thickness is very variable, and that in
some districts particular members of the series are wanting, or are
only slenderly developed. Still the section at the Joggins is by no
means an exceptional one, since I have been obliged to assign to the
Carboniferous deposits of Pictou, on the evidence of the sections
exposed in that district, a thickness of about 16,000* feet ; and Mr.
Brown has estimated the Coal-formation of Cape Breton, exclusive of
the Lower Carboniferous, at 10,000 feet in thickness+.

When fully developed, the whole Carboniferous series may be
arranged in the following subordinate groups or formations, the
limits of which are, however, in most cases not clearly defined :—

a. The Upper {Coal-formation.—It consists of sandstones, shales,
and conglomerates, with a few thin beds of limestone and coal. Cala-
mates Suckovi, Annularia galiordes, Cordartes simplex, Alethopteris
nervosa, Pecopteris arborescens, Dadoxylon materiarium, Lepidophloios
parvus, and Sigillara scutellata, are among its characteristic vege-
table fossils.

* Quart. Journ. Geol. Soc. vol. i. p. 329. tT Jbzd. vol. vi. p. 116.

1865. ] " DAWSON—COAL-FORMATION. on

b. The Middle Coal-formation, or Coal-measures proper.—This
series includes the productive beds of coal, and is destitute of pro-
perly marine limestones. Beds tinged with peroxide of iron are less
common in this formation than in any of the others. Dark-coloured
shales and grey sandstones prevail, and there are no conglomerates.
Sigillarie and Stigmarie of many species are the most conspicuous
and abundant fossils, but Ferns, Cordaites, and Calamites are also
extremely abundant, and all the genera of Carboniferous plants are
represented. Many beds, especially those in the vicinity of layers of
coal, contain minute Hntomostraca, shells of the genus Anthracomya
(Naiadites), Spirorbis carbonarius, and remains of ganoid and placoid
fishes.

e. The “ Millstone-grit” Formation.—This name, though not in
all cases lithologically appropriate, has been borrowed from English
geology to designate the group of sandstones, shales, and conglome-
rates, destitute of coal, or nearly so, and with few fossil plants, which
underlies the Coal-measures. In its upper and middle part it in-
cludes thick beds of coarse grey sandstone holding prostrate trunks
of coniferous trees (Dadoxylon Acadianum). ‘In its lower part red
and comparatively soft beds prevail.

d. The Lower Carboniferous Marine Formation.—The essential fea-
tures of this formation are thick beds of marine limestone, charac-
terized principally by numerous Brachiopods, especially Productus
Oora, P. semireticulatus, Athyris subtilita, and Terebratula sufflata*,
with other marine invertebrates. Associated with these limestones
are beds of gypsum, and they are enclosed in thick deposits of sand-
stone, clay, and marl, of prevailing red colours.

e. The Lower Carboniferous Coal-measures, or Lower Coal-
measures.—In some localities these resemble in mineral character
the true Coal-measures. In others they present a great thickness
of peculiar bituminous and calcareous shales. They usually contain
in their lower part thick beds of conglomerate, and coarse sandstone
which in some places prevail to the exclusion of the finer beds.
The characteristic plants of these beds are Lepidodendron corru-
gatum, and Cyclopteris Acadica, with. Dadoaxylon antiquius, and
Alethopteris heterophyllat. They also contain locally great quantities
of remains of fishes, and many Entomostracans, among which are
Leaa Leidyr and an Estheria, also Leperditia subrecta, Portlock,
Beyrichia colliculus, Kichw., and a Cytheret, probably new.

The last two groups are equivalent to the “ Sub-carboniferous ”
of some American geologists; but independently of the objection to
the use of a term which would seem to imply a formation under,
and distinct from, the Carboniferous, and of undetermined age, I find
in Nova Scotia no reason, either paleontological or stratigraphical,
for any greater distinction than that implied in the term Lower

* See Davidson ‘‘On Lower Carboniferous Brachiopoda from Nova Scotia,”
Quart. Journ. Geol. Soc. vol. xix. p. 158.

t Dawson, ‘On the Lower Coal-measures,” &c., Quart. Journ. Geol. Soe.
vol. xv. p. 62.

{ Prof, Jones has kindly determined these species.

98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

Carboniferous. The Lower Coal-measures are, it is true, more
distinct in their flora from the Middle Coal-measures than the latter
from the Upper Coal-formation ; but still many species are common
to the two former, and the difference is small as compared with that
between the Lower Carboniferous and the Upper Devonian. The
Devonian rocks are also in this region unconformable to the Carbo-
niferous, having been disturbed and altered prior to the deposition of
the latter; while no want of conformity, except of the local character
hereafter to be noticed, occurs in the Carboniferous.

2. Physical Conditions attending the Deposition{of the Coal-forma-
tions.—The conditions of deposit implied in the mineral character of
the several formations above described, would appear to be of three
leading kinds: —(1)The deposition of coarse sediment in shallow water,
with local changes leading to the alternation of clay, sand, and
gravel. This predominates at the beginning of the period, recurs
after the deposition of the marine limestones in the formation of the
“‘Millstone-grit,” and again prevails in the Upper Coal-formation.
(2) The growth of corals and shellfish in deep clear water, along
with the precipitation of crystalline limestone and gypsum. These
conditions occurred during the formation of the Lower Carboniferous
-Limestone and its associated gypsum. (3) The deposition of fine sedi-
‘ment, and the accumulation of vegetable matter in beds of coal and

carbonaceous and bituminous shale, and of mixed vegetable and

animal matters in the beds of bituminous limestone and calcareo-
bituminous shale. These conditions were those of the Middle Coal-
-formation.

Within the limits of Nova Scotia, these conditions of deposition ap-
-plied, not to a wide and uninterrupted space, but to an area limited
and traversed by bands of Silurian and Devonian rocks, already par-
tially metamorphosed and elevated above the sea, and along the
margins of which igneous action still continued, as evidenced by the
beds of trap intercalated in the Lower Carboniferous*; while about —
the close of the Devonian period still more important injections and _

-intrusions of igneous matter had occurred, as shown by the granitic
dykes and masses which traverse the Devonian beds, but have not
penetrated the Carboniferous}. There is evidence, however, in the
Carboniferous rocks of the Magdalen Islands and of Newfoundland,
and in the fringes of such rocks on parts of the coast of Nova
Scotiat and New England, that the area in question was only a part
of a far more extensive region of Carboniferous deposition, the greater
part of which is still under the waters of the Atlantic and of the Gulf
of St. Lawrence.

There is ample proof that most of the coarser matter of the Car-
boniferous rocks was derived from the neighbouring metamorphic
ridges; but much of the finer material was probably drifted from
more distant sources. There seems no good reason to doubt that in
the Carboniferous period, and especially in those portions of it in
* Dawson, Quart. Journ. Geol. Soc. vol. i. p. 329.

t+ Dawson, Canadian Naturalist, 1860, p. 142.
+ Jukes’s ‘Newfoundland ;’ ‘Acad. Geology,’ p. 274.

1865. | . DAWSON—COAL-FORMATION. ~ 99

which the areas now under consideration were in the condition of
shallow seas or swampy flats, the greater part of the Laurentian and
Silurian districts of North America existed as land; while the great
number of Coal-formation plants common to Europe and America
may indicate the existence of intermediate lands now submerged.
From such lands, undergoing waste during the long Carboniferous
time, the materials of the shales and finer sandstones may have been
derived.

Taking this view of the source of the sediment, we should infer
that the time of the formation of the marine limestones was that of
ereatest depression of the land, when the local ridges of older rock
were mere reefs and islets, and when sediment from more distant
lands was deposited only at intervals. We should also infer that the
time of the formation of the coal-beds was that of greatest elevation,
when the former sea-bottoms had become land-surfaces or flats,
exposed only to occasional inundation, and when rivers were bearing
downward from large continental regions great quantities of fine
silt. Further, the conditions of the Millstone-grit and of the Newer
Coal-formation must have been of an intermediate character, re-
quiring wide sea-areas receiving great quantities of sediment, and
on this account, as well as because of their shallowness, unfavourable
to marine life, while the areas of vegetable growth were also of

‘limited extent.

It would also follow that when the Lower Coal-measures and
conglomerates were formed, the land was slowly subsiding ; that in
the time of the marine limestones it attained to its greatest depres-
sion, and long remained nearly stationary; that in the Millstone-

grit period there was re-elevation, and that in the period of the
Middle Coal-formation and Newer Coal-formation there was again
subsidence, slow and interrupted at first, but subsequently of greater
amount. From the absence of Permian deposits it may be inferred
that elevation again took place at the close of the Carboniferous period,
to such an extent as to preclude further deposition in the area in
question ; while the red sandstone and trap of Mesozoic age indicate
the recurrence at that time of conditions somewhat similar to those
of the beginning of the Carboniferous period.

~The general phenomena of deposition above indicated apply to all
the Carboniferous areas of Nova Scotia and New Brunswick, and, so
-far as known, to those of the Magdalen Islands and of Newfoundland.
But, as I have pointed out in ‘ Acadian Geology,’ numerous local.
diversities occur, in consequence of the interference of the older
-elevated ridges with the regularity of deposition. In some places the
entire Lower Carboniferous series seems to be represented by con-
glomerates and coarse sandstones. In others, the Lower Coal-
measures, or the Marine Limestones, or both, are extensively deve-_,
loped. These local differences are, on a small scale, of the same
character with those which occur on a large scale in the Northern
and Southern Appalachian districts and Western districts of the United
States, and in the different coal-areas of Great Britain and Ireland,
as compared with each other and with the Carboniferous districts of

100 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Dec. 20,

America. On the whole, however, it is apparent that certain grand
features of similarity can be traced in the distribution of the Carbo-
niferous rocks throughout the northern hemisphere.

It is further to be observed that in Nova Scotia and New Bruns-
wick, as well as in Eastern Canada, disturbances occurred at the
close of the Devonian period which have caused the Carboniferous
rocks to lie unconformably on those of the former; and that in
like manner the Carboniferous period was followed by similar dis-
turbances, which have thrown the Carboniferous beds into synclinal
and anticlinal bends, often very abrupt, before the deposition of the
Triassic Red Sandstones. These disturbances were of a different cha-
racter from the oscillations of level which occurred within the Carbo-
niferous period. They were accompanied by volcanic action, and
were most intense along certain lines, and especially near the junc-
tion of the Carboniferous with the older formations,

I have noticed an apparent case of unconformability between
members of the Carboniferous system near Antigonish*. In the
county of Pictou the arrangement of the beds suggests a possible
unconformability of the Upper Coal-formation and the Coal-mea-
surest. In New Brunswick Prof. Baileyt has observed indications
of local unconformability of the Coal-formation with the “Lower
Carboniferous. But the strict conformability of all the members of
the Carboniferous series in the great majority of cases, shows that
these instances of unconformability are exceptional. In the section
at the Joggins, more especially, the whole series presents a regular
dip, diminishing gradually from the margin to the middle line of the
trough, where the beds become horizontal.

The most gradual and uniform oscillations of level must, however,
be accompanied with irregularities of deposition and local denuda-
tion; and phenomena of this kind are abundantly manifest in the
Carboniferous strata of Nova Scotia. I have described in ‘ Acadian
Geology’ a bed in the Pictou coal-field which seems to be an ancient
shingle-beach, extending across a bay or indentation in the coast-line
of the Carboniferous period§. At the Joggins many instances oceur of
the sudden running out and cutting off of beds ||, and Mr. Brown has
figured a number of instances of this kind in the Coal-formation of
Sydney4. They are of such a character as to indicate the cutting
action of tidal or fluviatile currents on the muddy or sandy bottom of
shallow water. In some instances the layers of sand and drift-
plants filling such cuts suggest the idea of tidal channels in an
estuary filled with matter carried down by river-inundations. yen
the beds of coal are by no means uniform when traced for consider-
able distances. The beds which have been mined at Pictou and the
Joggins show material differences in quality and associations; and
small beds may be observed to change in a remarkable manner, in

* Quart. Journ. Geol. Soc. vol. i. p. 32.

+ Ibid. vol. x. p. 42; Acadian Geology, p. 249.

t Report on Geology of Southern New Brunswick, p. 118.

§ Quart. Journ. Geol. Soc. vol. x. p. 45, || Zdéd. vol. x: p. 12.
| Ibid. vol. vi. p. 125 e¢ seg.

1865. ] DAWSON—COAL-FORMATION. 101

their thickness and in the materials associated with them, in tracing
them a few hundreds of feet from the top of the cliff to low-water
mark on the beach. I have no doubt that, could we trace them
over sufficiently large areas, they would all be found to give place to
sandstones, or to run out into bituminous shales and limestones,
according to the undulations of the surfaces on which they were
deposited, just as the peaty matter in modern swamps. thins out
toward banks of sand, or passes into the muck or mud of inun-
dated flats or ponds.

3. Geological Cycles.—The foregoing considerations bring,in a very
distinct manner, before us two different, and at first sight irreconcile-
able, general views which we may take of any given geological period.
Firstswe must regard every such period as presenting during its whole
continuance the diversified conditions of land and water with their
appropriate inhabitants; and secondly, we must consider each such
period as forming a geological cycle, in which such conditions to a
certain extent were successive. As we-give prominence to one or
the other of these views, our conclusions as to the character of geo-
logical chronology must vary in their character; and in order to
arrive at a true picture of any given time,.it is necessary to have
both before us in their due proportion.

We know that the marine“animals of the Lower Carboniferous.seas
continued to exist in the time of the Coal-formation, and that some
of them survived until the Permian period, proving to us the exis-
tence of deep seas even in that age which we regard as specially
characterized by swampy flats supporting land-plants. In like man-
ner we know that some of the species of land-plants found in the
lowest Coal-measures continued to exist in the time of the Upper
Coal-formation, proving that there was some land suitable for them
throughout the epoch of the deep-sea limestones. Regarded from
this point of view, any exceptional beds with land-plants in the
marine parts of the formation, or beds with sea-shells in the parts
where land-conditions predominate, acquire a special interest; and
so likewise do regions in which, as in some parts of the Appalachian
Coal-field, the marine limestones are absent, and those in which, as
in some parts of the Western States, marine conditions seem to have
continued throughout the whole period. In Nova Scotia, so far
as my present knowledge extends, the marine limestones of the
Lower Carboniferous cut off the flora of the Lower Coal-measures,
apparently by a long interval of time, from that of the Middle Coal-
formation ; and in like: manner the fossils of the marine limestones
cease at the time of the Millstone-grit, and only in one instance,
that of a small bed of limestone near Wallace Harbour, partially re-
appear in the Upper Coal-formation*. .I have, however, ascertained
that the Marine Limestones may be divided into an upper and a
lower member, and that there is some reason to suppose that in
some parts of Nova Scotia, where the true Coal-measures are not
developed, the. upper member may in part, at least, represent them.

* Acad. Geol. p. 183; Quart, Journ. Geol. Soe. vol. ii. p. 133.

Tt Quart. Journ. Geol. 'Soe. vol. xv. pp. 63 e¢ seg. My friend Mr.C. F. Hartt, who
VOL, XXII,—PART I, I

102 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 20,

On the other hand, I have not as yet been able to bridge over the
gulf which separates the flora of the Lower Carboniferous Coal-
measures from that of the Middle Coal-formation, an interval which
may include much of the “ Lower Coal-measures” of Rogers in the
Pennsylvania Coal-field.

Turning to that broader view which takes the prevalent conditions
of each portion of the period as characteristic, notwithstanding the
local existence of dissimilar conditions, we not only find, as already
stated, that the sequence in Nova Scotia coincides generally with
that in other parts of America and in Europe, but that, viewed in
this aspect, the Carboniferous period constitutes one of four great
physical cycles, which make up the Paleozoic age in Hastern
America—and each of which was characterized by a great substlence
and partial re-elevation, succeeded by a second and very gradual
subsidence. Viewed in this way, the Lower Carboniferous conglo-
merate and Lower Coal-measures correspond analogically with the
Oriskany Sandstone, the Oneida and Medina Sandstones, and the
Potsdam and Calciferous. The Carboniferous Limestone corresponds
with the Corniferous Limestone, the Niagara Limestone, and the
Trenton group of limestones. The Coal-measures correspond with
the Hamilton group, the Salina group, and the Utica Shale. The
Upper Coal-formation corresponds with the Chemung, the Lower
Helderberg, and the Hudson-River groups. The Permian is not
represented in Kastern America; but as developed in Europe it
clearly constitutes a similar cycle. These parallelisms, which deserve
more attention from geologists than they have yet received, may be
tabulated thus * :— ;

Tabular View of Cycles in the Paleozoic Age in Eastern America, —
(The several formations are arranged in descending order.)
, Carbo-

niferous.

——

Lower Upper
Silurian. Silurian.

Character of group. Devonian.

Hudson-River |Lower Helder-|Chemung gr... Dynes Coal-

area, filling up with sedi-
group. berg group. ormation.

Shallow, subsiding ied |
gubeidence, land-surfaces,| } Utica shale ..|Salina group. .|Hamilton gr. ..|Coal-mea-
CULT ARR ASIAN 6 Une 3 sures.
Trenton, Black|Niagara and |Corniferous |Lower Carbo-

ae or ee ee Be andChazy| Clinton limestone. | niferouslime-
imestones. limestones. stone.

Subsidence ; disturbances ;|\ Potsdam and/Oneida and |Oriskanysand-|Lower Coal-

_ deposition of coarse sedi- Calciferous | Medina stone. measures and

baiY2) 61 Pe hScint ante Clo; Srearicioc sandstones. sandstones. conglomerate.

Ts the Permian of Europe, the Stinkstein, the Rauchwacke, the
Zechstein, and the Rothliegendes might form a fifth parallel column.

has more recently studied the Marine Limestones, has obtained facts which seem to
indicate the possibility of a more minute subdivision than any hitherto attempted
of these beds.

* Dr. Sterry Hunt has directed attention to them in a paper “ On Bitumens,”
‘Silliman’s Journal’ [2], xxxv. p. 166, and in the ‘ Geology of Canada,’ 1863,
p. 627 ; and Dana refers to them in his ‘Manual of Geology.’ Eaton and Hall
had previously noticed these parallelisms.

1865, | DAWSON—COAL-FORMATION, ° 103

Of course such parallelism might be variously expressed by reckon-
ing a smaller or larger number of groups. Independently of these
different modes of statement, however, I believe that the basis of
such comparisons exists in nature, and that it will prove possible to
subdivide geological time into determinate natural cycles, the parts
of which are analogous to those of similar cycles. A further question
to be solved is, whether such cycles corresponded in all parts of the
world, or whether, as is more likely, the earth might be divided into
areas in which in each cycle elevation and subsidence were contem-
poraneous. So far as the present subject is concerned, I merely
desire to show that the Carboniferous rocks of Nova Scotia represent
a complete cycle of the earth’s history, and correspond in time with
the Carboniferous of Europe, and in value with the other great
divisions of the Paleozoic age.

_ 4. Summary of facts relating to the mode of accumulation of Coal.
—wWith regard to the more special subject of this paper, I would
rather invite attention to the details to be presented under the next
head, than make any preliminary general statements. It is, how-
ever, necessary to notice here the several views which have prevailed
as to the probable accumulation of coal by driftage or growth im
situ, in water or on land. I have already, in previous publications*,
stated very fully the conclusions at which I have arrived on some
portions of this subject, and I would now sum up the more import-
ant general truths as follows:—(1) The occurrence of Stigmana
under nearly every bed of coal, proves beyond question that the
material was accumulated by growth i in situ, while the character of
the sediments intervening between the beds of coal proves with
equal certainty the abundant transport of mud and sand by water.
In other words, conditions similar to those of the swampy deltas of
great rivers are implied. (2) The true coal consists principally of
the flattened bark of Sigillarioid and other trees, intermixed with
leaves of ferns and Cordaites, and other herbaceous débris, and with
fragments of decayed wood constituting ‘mineral charcoal,” all
these materials having manifestly alike grown and accumulated
where we find them. (38) The microscopical structure and chemical
composition of the beds of Cannel-coal and earthy bitumen, and of
the more highly bituminous and carbonaceous shales, show them to
have been of the nature of the fine vegetable mud which accumu-
lates in the ponds and shallow lakes of modern swamps. When
such fine vegetable sediment is mixed, as is often the case, with
shales, it becomes similar to the bituminous limestone and calcareo-
bituminous shales of the Coal-measures. (4) A few of the under-
clays which support beds of coal are of the nature of the vegetable
mud above referred to; but the greater part are argillo-arenaceous
in composition, with little vegetable matter, and bleached by the
drainage from them of water containing the products of vegetable
decay. ‘They are, in short, loamy or clay soils, and must have been
sufficiently above water to admit of drainage. The absence of sul-

* “On the Structures of Coal,” Poa Journ. Geol. Soc. vol. xv. Air-breathers —
of the Coal Period, Moutreal, 1863, p. 1
12

104 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 20,

phurets, and the occurrence of carbonate of iron in connexion with
them, prove that, when they existed as soils, rain-water, and not sea-
water, percolated them. (5) The coal and the fossil forests present
many evidences of subaérial conditions. Most of the erect and
prostrate trees had become hollow shells of bark before they were
finally imbedded, and their wood had broken into cubical pieces of
mineral charcoal. lLand-snails and galley-worms (Xylobius) crept
into them, and they became dens or traps for reptiles. Large quan-
tities of mineral charcoal occur on the surfaces of all the larger beds
of coal. None of these appearances could have been produced by
subaqueous action. (6) Though the roots of Szgillaria bear some
resemblance to the rhizomes of certain aquatic plants, yet structu-
rally they are absolutely identical with the roots of Cycads, which
the stems also resemble. Further, the Sigillarie grew on the same
soils which supported Conifers, Lepidodendra, Cordaites, and Ferns,
plants which could not have grown in water. Again, with the ex-
ception, perhaps, of some Pinnularie and Asterophyllites, there is a
remarkable absence from the Coal-measures of any form of properly
aquatic vegetation. (7) The occurrence of marine or brackish-
water animals in the roofs of coal-beds, or even in the coal itself,
affords no evidence of subaqueous accumulation, since the same thing .
occurs in the case of modern submarine forests. For these and
other reasons, some of which are more fully stated in the papers
already referred to, while I admit that the areas of coal-accumu-
lation were frequently submerged, I must maintain that the true
coal is a subaérial accumulation by vegetable growth on soils wet
and swampy, it is true, but not submerged. I wouid add the further
consideration, already urged elsewhere, that, in the case of the fossil
forests associated with the coal, the conditions of submergence and
silting-up which have preserved the trees as fossils must have been
precisely those which were fatal to their existence as living plants—
a fact sufficiently evident to us in the case of modern submarine
forests, but often overlooked by the framers of theories of the accu-
mulation of coal.

It seems strange that the occasional inequalities of the floors of
the coal-beds, the sand or gravel ridges which traverse them, the
channels cut through the coal, the occurrence of patches of sand,
and the insertion of wedges of such material splitting the beds, have
been regarded by some able geologists as evidences of the aqueous
origin of coal. In truth, these appearances are of constant occur-
rence in modern swamps and marshes, more especially near their
margins, or where they are exposed to the effects of ocean-storms or
river-inundations. The lamination of the coal has also been
adduced as a proof of aqueous deposition; but the microscope shows,
as I have elsewhere pointed out, that this is entirely different from
aqueous lamination, and depends on the superposition of successive
generations of more or less decayed trunks of trees and beds of
leaves. ‘The lamination in the truly aqueous cannels and een
~ naceous shales is of a very different character.

It is scarcely necessary to remark that in the above summary I

1865. ] DAWSON-—COAL-FORMATION, 105

have had reference principally to the appearances presented by the
Coal-formation of Nova Scotia, and that I have no wish to under-
value the admirable researches on this subject of Brongniart,
- Goeppert, Hawkshaw, Beaumont, Binney, Rogers, Lesquereux, and
others, whose publications on this subject I have read with interest,
and have tested in their application to the phenomena presented to
me in the coal-fields of Nova Scotia. I may add that in my opinion
the phenomena of the Stigmaria-underclays, to which attention was
first directed by Sir W. E. Logan, furnish the key to the whole
question of the origin of coal, and that the comparisons of Coal-
‘deposits, by Sir Charles Lyell, with the ‘“‘ Cypress-swamps” of the
Mississippi perfectly explain all the more important appearances in
the Coal-formation of Nova Scotia.

§ II. Derarts of tor CHARACTER AND Fossit ConTENTS OF THE SEVERAL
Brps or Coab, AS EXPOSED IN THE SoutH Jogerns SEcTION.

1. Jntroduction—-Under this heading I propose to state all the
facts bearing on the origin and mode of formation of the several coals,
obtained either by careful study of their outcrops on the ground, or
by subsequent examination, with the aid of the microscope, of speci-
mens collected from them. I shall follow the order of the detailed
section published by Sir W. E. Logan in 1845*, including the ad-
ditional points observed by Sir C. Lyell and myself in 1852, and by
myself in several successive visitst, but giving in minute detail only
the coals and their associated roof-beds and underclays. The sand-
stones and shales which constitute the mechanical filling-in between
the beds of coal I shall group together in the shortest possible manner,
referring to the published sections above-mentioned for details. I
shall, however, mention every case of the occurrence of beds holding
erect trees, and of Stigmarian underclays, as well as of beds of bitumi-
nous limestone and highly carbonaceous shale. I regard the former as
- being truly land-surfaces, as well as the coals, and the latter as
accumulations of vegetable mud or muck which imply the contem-
poraneous existence in their vicinity of swamps and forests.

2. Logan’s Section (order descending). a. Division 1.—This ex-
tends along the coast from Shoulie River to the vicinity of Ragged
Reef, being nearly horizontal at the former place and gradually
assuming a decided south-west dip towards the latter. It is 1617
feet in vertical thickness, and constitutes the upper part of the
“‘ Upper Coal-formation.” It occupies the centre of the great syn-
clinal of the western part of the Cumberland coal-area, and presents
the newest beds of the Carboniferous system.

The rocks are thick-bedded white and grey sandstones, passing
in some places into conglomerates with quartz pebbles, and inter-
stratified with reddish and chocolate shales. The sandstones pre-
dominate.

Fossils are not numerous in these beds. Those found are Dadoxy-

* Report of Progress of Canadian Survey, 1845.
t+ Quart. Journ. Geol. Soc. vol. x.; also Acadian Geology, p. 128 e¢ seg.

106 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. f Dec. 20,

lon materiarium, of which there are many drifted trunks in the sand-
stones in a blackened and calcified condition, Calamites Suckovi,
C. Crist, Calamodendron approaimatum, Lepidodendron undulatum,
Lepidophloios parvus, and Stugmaria ficoides. As in the Upper Coal-
formation of Pictou, trunks of Conifers and Calamites are the most
abundant fossils.

b. Division 2.—This occurs at Ragged Reef and its vicinity. Its
thickness is 650 feet. It constitutes the lower part of the Upper
Coal-formation.

The rocks are white and grey sandstones with occasional reddish
beds, and red and grey shales. The sandstones and shales are nearly
in equal proportions. Underclays, or soils supporting erect aa
probably Stgillarie, occur at two levels.

Fossils are not numerous. Those collected were Sigillaria scu-
tellata and Stigmaria ficordes, Calamites Suckovir, Sphenopteris
hymenophylloides, Alethopteris lonchitica, Cyclopteris heterophylla (?),
Beinertia Goepperti, and portions of the strobiles of two species of
Lepidophloios, namely Lepidophyllum lanceolatum and L. trinerve.

c. Division 3.—This extends in descending order from the vicinity
of Ragged Reef to M*Cairn’s Brook. Its thickness is 2134 feet. It
includes the upper part of the ‘‘ Middle Coal-formation,” and is
perhaps equivalent, in part at least, to the Upper Coal-measures of
Great Britain, and to the Upper Coal-formation of American authors.

It includes 1009 feet of sandstone, almost all of which is grey,
and 912 feet of grey and reddish shale and clay. It contains 22
beds of coal, all of small thickness, and most of them of coarse
quality. Below I give each bed of coal in detail, with its roof and
floor and its fossils; and the intervening mechanical beds in brac-
kets. ‘The thickness of the roofs and floors is included i in that stated
for the intervening beds.

ft. in.
(Carbonaceous shale, grey understone, with Stigmaria
and: grey shale) ....c./.c0ceasssegvcsersdo. ta eae ve eaeee 7 0
Grey argillaceous shale.
Coal group L veoh Coat 1 inlis se. cp venue vactemSer anae9eeae eg aeanaeereas Ns sit O. A
Grey argillaceous underclay, Stigmaria. 5 ae
The roof holds abundance of Alethopteris lonchitica. The
coal is coarse and earthy, with much epidermal and_ bast
tissue*, vascular bundles of ferns, and impressions of Szgal-
laria and Cordaites. It is a compressed vegetable soil or
dirt-bed, resting on an argillaceous subsoil with rootlets of
Stigmaria.
(Grey and reddish sandstones and grey and red shales
with ironstone NOGUIeS)..4. a0. ess seqses orice res eee 281 6
( Reddish argillaceous shale.
. Coal TUCH a vines. Beeswss ues
Coal-group 2 ...{ Carbonaceous shale 4 inches... | ....c...cecesseseeesaeee 0 6

Coal IW inclin nanny sce aoe
Reddish underclay, Stzgmaria.

* For explanation as to the nature of these and other structures in the coal,
see under § IV., below.

1865.] . -*« DAWSON—-COAL-FORMATION,

The coal is coarse, earthy, and shaly. It contains Cor-
daites, fern stipes, and bast tissue.

(Reddish shale and grey sandstone, the latter seen in

the cliff to thin out and give place to reddish shale)
Grey sandstone.

| Coat 1 wielass.4 tia .ss scans sesssaances steaanadav de. sentaos .

Coal-group 3 ...
Grey and reddish sandy understone, S¢igmaria.

The coal is coarse and shaly. No fossils were observed,
except stumps and rootlets of Stgmaria in the underclay.
(Reddish grey shale and grey sandstone) ...............
Reddish grey shale.
Roml-sroups iee4 Coal 2 inches... .cscsaicssssvesdeccdabesssaeavsaseeceesescess
Grey and reddish argillaceous underclay, Stigmaria.
The coal is coarse and earthy. No fossils were observed,
except Stgmaria rootlets in the underclay. This and the
last coal are to be regarded merely as fossil vegetable soils
or dirt-beds.
(Grey sandstone and grey and reddish shale. One
underclay, and erect Calamites in the lowest bed)

Grey argillaceous shale.
BPA rae. 4) COML INCHES... .c.sccsnsecsossessscccersscugensuetsesnacon ee

Grey argillo-arenaceous underclay, Stigmaria.
The coal is filled with leaves of Cordaites borassifolia,
dividing it into thin papery layers. The underclay has
many large branching roots of Stigmaria.

(Grey shale and sandstone) .......00......seseeaee ee isa cses
Grey arenaceous shale.
Piretieeronp i 6. Codl S INChesd 6.0.60 ec ce ceca bessscccnstedeasseccccscsese
| Grey argillo-arenaceous underclay, Stigmaria.

This coal is composed of flattened bark of Sigillaria, of

which there are many layers in the thickness of the bed.

The species are not distinguishable.

(Grey sandstone and shale. One underclay with
ISELG MERIC). site echo tee amare hah take Sao comsjsien «
/ Grey argillaceous shale.
Coal 1 inch.
Grey argillacous underclay, Stigmaria, 1 ft. 6 mn.
Coal-group 7 ... 4° Coal 2 inches. -
Grey argillaceous underclay, Stigmaria, 4 inches.

Coal 1 inch.
Grey argillaceous underclay, Stigmaria .......1....068
This is an alternation of thin coarse coals or fossil vege-
table soils with Stigmaria subsoils. The roof-shale con-
tains erect Calamites, which seem to have been the last
vegetation which grew on the surface of the upper coal.
(Grey and reddish sandstones and shales) ..............-
Red and grey shale.
BGI. Wale UMM tenn tic Racca teas wat cahtiileg «46 +8 ECBpeUT
Grey hard underclay, Stigmaria.
This coal contains flattened trunks of Stgilaria scutel-
lata, or an allied species, and of other Szgillaric, also

Coal-group 8 ...

239 6

19 0

12 6

108 PROCEEDINGS OF THE GEOLOGICAL society. [Dec. 20,

abundance of vascular bundles of ferns and portions of
epidermal tissues of different plants.

(Grey sandstone and red and grey shales. S¢igmaria
in the upper bed, and prostrate Sigillaria and
Cordaites in some of the sandstones and shales)...
Grey argillaceous shale, ironstone nodules.
Coal-group 9 . a Coal: inehes wie. cesaaendeaete ate Rene Waist rans
Argillo-arenaceous underelay, Stigmaria.

The roof of this coal holds prostrate Sigillarie of three
species and Cordaites borassifolia. ‘The coal is hard and
shining, with impressions of flattened Sigillarie, also of
Cordaites, Asterophyllites, Carpolites, and vascular bundles
of ferns.

(Underclay and reddish grey shale) ..........4.. sae daiee
Reddish grey shale.
Coal and coaly shale 8 inches.
Grey argillaceous underclay, nodules of ironstone,
and “Stigmari ia 2 feet.
| Coal, stony and compact, 2 inches ...........sscsseeees
\ Grey argillaceous underclay, Stigmaria.

Coal-group 10.. a
|

The roof-shale has obscure impressions of plants, appa-
rently petioles of ferns. The upper coal is thinly laminated
and full of leaves of Cordaites and ferns, among which is
Alethopteris lonchitica. The lower coal is compact, resem-
bling cannel, and has many vascular bundles of ferns. It
seems to be composed of herbaceous matter macerated in
water and mixed with mud.

(Grey sandstone and shale with nodules of ironstone)
Grey argillaceous shale.
Coal-group 11... | Codi estiallivgy es TaN CME Sie mece emmasereeiin ere swine
Arenaceous underclay, Stigmaria.

An erect ribbed Sigillarza appears in the roof-shale. The
coal contains many flattened Sigillamie, also Trigonocarpa,
Cordaites, and vascular bundles of ferns.

(Arenaceous understone with ironstone voile and
Stigmaria, and carbonaceous shale)......... jsaeeee
f Carbonaceous shale.
Coal-group 12... Coal’ ices 02. ..20..-.. sn seaee sade) ah ene eee eee
Saeatbeeos underclay, ironstone, and Stigmaria.

This coal is hard and laminated, with many ees
bundles of ferns upon its surfaces. .

Coal-group 13... 1 ee Coal 7 inches it as deena uadne at ha gaan asus ceacan tte a eeeRen

Grey argillaceous underclay, ironstone, and Stigmaria.

The roof contains erect stumps, not distinctly marked.
The coal has indications of bark of Sigillaria, and is hard
and shining, with a coarse earthy layer in the middle.

(na(Gkeyishale) “i. .idimucsdscare a ee Be

Grey shale, as above.
Coal-group 14... aie: inches ..,... eeedenens esunescenss sfhasshrusddpansaess

£5 Ins

490 0
0 3

2 10

1865. ] DAWSON-——COAL-FORMATION,

Coal-group 14... 4 Grey argillo-arenaceous underclay, ironstone, and
PSULAMOTT, . . s esinssasalee Ailes Tae eceme states amen seer aen Le
f CGO ATICIVCR, «om sac. seis maw oo Sere acto seletra seam esata ate asees

The upper coal has impressions of bark of trees and
Cordaites, especially in its upper part.
(Grey and reddish shale and grey sandstone, with Stig-

marian soils at two levels) .........eseseseee aewazaren
Grey shale.
Carbonaceous shale 2 inches.
Coal-group 15...< Argillaceous underclay, ironstone, and S¢zgmaria...
Capa UE NNIEG Wie to 8 swiss Sescde rie ae se wna Resagtentejp oh Eolenins « eoinn a

Argillaceous underclay, ironstone, and Stzgmaria....

The upper shaly bed is a coal interlaminated with shale,
which enables the nature of the coaly matter to be ascer-
tained. It contains flattened Sigillariw of several species,
Calamites, Cordaites, Cyperites, leaves of Sigillaria, and
Lepidophylla. ‘The clay parting is the roof of the lower coal,
and contains Oyperites and Cordaites. It has been converted
into an underclay by the growth of Stgillarza upon it in
the formation of the upper bed of. coaly shale. The lower
coal is compact, but showed an impression of a Calamite.
(Grey sandstone and grey and reddish shale, ironstone

MOM NES) Ps cok Ma tacea tee dens’ mi aintatsitats ahianstun estfenwiaaiah Se

Grey argillaceous shale.

Coal and carbonaceous shale 2 inches..............000

Reddish argillaceous underclay, ironstone, and Stig-

maria.

The roof supports an erect tree, a Sigillaria 8 feet high
and 1 foot in diameter. It is also rich in Cyperites*, Cor-
daites, and Calamites. The coal contains Calamites and
and also discigerous tissue of Conifers or Sigillaria.

(Grey sandstones and reddish and grey shales, with
several Stigmarian underclays and coaly films or
thin vegetable soils. One of the underclays sup-
ports large’ stumps of Sigillaria, with Cyperites,
- Cordaites, and Lepidodendron in the bed around
their bases) FPice beats op aide auimaehsie GMeniideae nels sioinia wa

Red and grey argillaceous shale.
Coal 1 inch.
Gray argillo-arenaceous underclay, St¢gmaria, 4 ft.
Coal-group 17... 4 Coad 4 inches.
| Carbonaceous shale 4 inches.
COG VANE i cna dncate seen seieneseass elise oe Uawilereniewge
\ Grey arenaceous underclay, "Stigmaria.

The upper layer of coal consists in part of leaves of Cor-

Coal-group 16...

daites. The middle layer has much Cordaites and Cyperites.

(Underclay and grey shale) ............+4 eeleaie a wreisiastaies
Grey shale, as above.
Barrow 1Sin a) Com Sanches. 65.5. csicnuttinnsensanadiaba sed anainele ne ceniiceee
Grey arenaceous underclay, Stigmaria.

Grey argillaceous underclay, ironstone, and Stigmaria.

52 0

on
woe

16 0
O° 2

PbO)

* By this term I continue, fee convenience, to designate the leaves of Sigii-

larie.

110 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 20,

"(Grey sandstone, and red and grey seks Stigmarian
soils .ab. two leyels) svavesn wnt ea GIGS des. sen sncole seaaeee
Reddish shale. ‘
Coal-group 19... Coad 1 ineli. i: ct chennesandtceh suas ivevasi iti oeesteiceees
Red argillaceous underclay, Stigmaria.

The roof contains an erect Sigillaria. The coal and that
of the previous bed were not well seen. |
(Grey sandstone and red and grey shales, with many
drift-trunks and erect Stgil/arie at four levels)...

Grey shale.

Coal-group 20.:: 5 Coat I imelist:..ic2-aeueccsaes:-2.ts1eesasecaserdosyen sieecena
. Red and grey underclay, Stigmarid.......1.ssecoeseeee

This coal contains much Cordaites.

(Grey and red shales and grey sandstone. One Stig- -

marian soil, and resting on it carbonaceous shale
with Cyperites) Danita pealge ose sal gems'v ie oagattean ae
( Grey shale.
Coal 2 inches.
Underclay, Stigmaria, 2 inches.
Coal-group 20a* { Coal 1 inch.
Underclay 1 inch, Stégmaria. ;
Coal 3 mches.: :...0.c80scs<se0: deste sien Woes. ae Pee
\ Argillaceous underclay, ironstone, and Stigmaria.

These coals contain mineral charcoal, showing scalari-
form and epidermal tissues.. The coals are impure, and were
probably concealed at the time of Sir W. KE. Logan’s visit.

(Sandstone and red and grey shale, with one See
HiaM. SOIL)... oc.ccisiaassiceie’ caleep eM ENR eae Re eee
; Red shale.
Coal-group 21... 4 Coal and carbonaceous shale, 2 inches....... ds seouusnne
Grey argillaceous underclay, Stiqmaria.

In the bed above the roof-shale are erect Calamites.
The coal is an uneven or-irregular bed, and consists of
flattened Srgillaric, Cyperites, Cordaites, and ferns.

(Grey and reddish sandstones and shales, with drift-
trunks of Dadoxylon materiarium, Sigillaria, and
Calamilesy nasszrewitsesviznt tn yisd tiene toe Soene eee
Grey and red shale, nodules of ironstone.
Coal-group 22... Coat and carbonaceous shale, 2 inches ...............
Grey argillo-arenaceous underclay, Stigmaria.

This coal consists of flattened. bark of Siqiularva with
Cordaites, and vascular bundles of ferns. It contains also
remains of fishes. Among these was found a tooth of Cte-
noptychius. The underclay includes stumps of Stegmaria,
as well as rootlets.

(Grey sandstone and shale with one Stigmarian soil
supporting erect stumps of S7gillaria)........0...066

Total thickness of Division 3, according to Logan’s measurements.....

ft. it
26

222

16

93

334

0
i

. 2159 8

d. Division 4.—This division of the section extends from M°Cairn’s
Cove to the end of the high cliff beyond “ Coal-mine Point.”

* T designate in this way coal-groups not noticed in Logan’s section.

It

1865.) ._ .... | DAWSON—COAL-FORMATION, ——- Lik

corresponds to the lower part of the Middle Coal-formation, and
probably to the Lower Coal-formation of some American authors.
Its thickness, according to the measurements of Sir William E. Logan,
is 2539 feet. It is remarkable for the prevalence of grey sandstones
and grey and dark-coloured shales. It constitutes the part of the
section re-examined by Sir C. Lyell and myself in 1852; and in the
memoir which I subsequently published it is divided into 27 groups
or subdivisions. For facility of reference these groups are indicated
by the Roman numerals in the following pages, beginning with the
highest group, XXVII.

BEY > XXVIII.
Bituminous limestone and calcareo-bituminous shale 't i-
2 ae | 4 feet.
ee Es EY Cont foot issecaiasset S coavdanvalteravecsaus doWlers inet nudes 5 0
Grey argillo-arenaceous underclay, Stigmaria.
The roof has Nazadites carbonarius and N. elongatus, Spi-
rorbis carbonarius, scales of Rhizodus, and obscure vege-
table fragments. The coal contains flattened Sigillaria, .
Cordaites, Alethopteris lonchitica, Cyperites, Calamites Nova-
scotica, and many vascular bundles of ferns.
(Grey sandstone and shale with six underclays and
erect Sigzllaria at two levels; also a thin shale
with Natadites, Cythere, Calamites, and Cordaites.
One of the sandstones has scales and teeth of a
large fish (? Rhizodus) and plants covered with
PEC OTM sagan aea rhein dase Ben sadebgn de eiscsoxdcveis 50 0
( Grey argillaceous shale.
Coal 1 inch.
Clay 3 inches,
Coal 1 inch.
Coal-group 2...4 Clay 1 inch.
Coal 1 inch.
‘| Shale 4 inches.
CSP ea TINNED gps s¥cs caves ic Maya ted stay sedgbeedeere chee eg

Grey argillo-arenaceous underclay, Stigmaria,

The roof has numerous vegetable fragments and flat-
tened Stgillarie and Calamites. One of the coals contains
mineral ¢harcoal, showing bast tissue, scalariform tissue,
and fragments of epidermis. The lower coal has bark of
Sigillaria, Stigmaria, and Cyperites, also numerous T'rigo-
nocarpa and vascular bundles of ferns. The clay partings
and the underclay have obscure rootlets, probably of Stig-
maria. —

(Arenaceous underclay and shale with remains of
Stigmaria.)
Grey argillaceous shale.
Coal-group 3... COab.3 MUGHESic ute renames tant Addouseesdleesoathecves isa 0 3
Hard argillo-arenaceous underclay, Stigmaria.

The roof has stumps of Sigillarie, erect and with roots —
of Stigmaria descending among them from the bed above.
The coal, which is coarse and earthy, has vascular bundles
of ferns, scalariform vessels, bast tissue, and scales and

112 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

spines of fishes (Palwoniscus, &c.), with coprolitic matter. ft. in.
The underclay shows abundant Stigmarian rootlets.
(Underclay and grey arenaceous shale).....:.0ses.0.++ 6 0
Grey argillaceous shale.
Coal 9 inches.
Carbonaceous shale 6 inches.
Coal 1 inch.
Carbonaceous shale 4 inches.
Coal-group 4...{ Coal 1 inch.
Carbonaceous shale 8 inches.
Coal 2 inches.
Grey shale 1 foot 7 inches.
CoG BANCHeS Mn tesa Oee tae ta onnuecianaot soememtie sajeine 410
| Argillo-arenaceous underclay, Stigmaria.
The roof contains obscure flattened plants. The coal is
hard or shaly, with vascular bundles of ferns and bast tissue.
The carbonaceous shales yield Cordaites borassifolia, Ale-
thopteris lonchitica, Calamites, Sigillaria, and Cyperites.
The grey shale parting has erect stumps, apparently of
Sigillaria. The upper shales and coals are very pyritous,
and decompose when exposed to the weather—an indication
that sea-water had access to these beds while the vegetable
matter was still recent.
XV.
(Grey argillaceous sandstone and red and grey shale,
with two Stigmarian soils. Footprints, probably
of Dendrerpeton, and rain-marks occur in these
beds; and it was in one of them that Mr. Marsh
discovered the vertebree of Hosaurus Acadianus). 82 O

XXY.

Bituminous limestone 2 feet.

Coal 3 inch.

Argillo-arenaceous clay, S¢¢gmaria, 6 inches.

Coaly shale 4 inch.

Grey argillo-arenaceous shale, ironstone nodules,
Stigmaria, 1 foot 6 inches.

Coaly shale \ inch.

Grey shale, ironstone nodules, S¢t¢gmaria, 2 ft. 6 in.

Codl G JNCWES +... ssniidacioccanter > Haast none Ube eee eee sas 7 2

Argillo-arenaceous undercelay, S¢igmaria.

The bituminous limestone of the roof contains Naiadites
carbonarius and LV. elongatus, fish-scales, and Cyprids. The
upper layer of coal contains impressions of Szgzllaria and
Lepidodendron, on some of which are shells of Spzrorbis.
It has epidermal tissues, vascular bundles of ferns, and re- |
ticulated vessels. ‘The coaly shales are of the nature of
coarse coals, but with numerous thin layers of shaly matter.
The lower coal contains petioles of ferns and Cordattes matted
together, and numerous Cardiocarpa. The two thick clay
partings and the underclay are Stigmarian soils.

Coal-group 5...

XXIV.

(Grey sandstone and chocolate and grey shales, with
LWOMSUSMBLIAM SOME)” cravcstne seavensascewenweneeittte 147 0

1865. ] DAWSON—COAL-FORMATION,

XXIII.

Carbonaceous shale, passing downward into bitu-
minous limestone, 1 foot 10 inches.
Coal-group 6... GAUL CHeS) sais inh. Bocca jou sooed aneeee ck oka nee

Argillo-arenaceous underclay, Stigmaria.

The roof contains Naiadites carbonarius, Cythere, Spi-
rorbis, fish-scales, and coprolites. The coal is hard and
laminated, and has on its surfaces leaves of Cordaites and
vascular bundles of ferns. It is remarkable for containing
scattered remains of a number of species of fishes, belonging
to the genera Ctenoptychius, Diplodus, Paleoniscus, and
Rhizodus. The underclay has rootlets of Stigmaria, and
the bed below this has large roots of the same.

(Grey sandstone and shale, the latter with nodules of
ironstone. Erect trees at one level) .........s0000
( Grey sandstone.
Coal 10 inches.
Carbonaceous shale 2 inches
Coal-group 7 | Coal 10 inches.
: Carbonaceous shale 2 inches.
Coal and coaly shale 2 feet 6 inches. ...ccssssecees “secs
Grey argillo-arenaceous underclay, Stigmaria.

This is the bed worked at the Joggins as the “ Main
Seam ;” and I believe that it improves somewhat in mining
it inward from the shore. The roof has afforded Sigillaria
catenoides and other species, Alethopteris lonchitica, Cor~
daites borassifolia, Lepidodendron elegans, Trigonocarpa,
Naiadites, Spirorbis, Cythere, fragments of insects (?). ‘The
mineral charcoal contains bast tissue, scalariform, epi-
dermal, and cellular tissues. In the compact part of the
coal there is dense cellular and epidermal tissue. The roof
is especially rich in Cordaites, sometimes with Spirorbis
adherent.

(Grey sandstone and shale, with many ironstone
nodules in the shale, and erect Sigil/arta and un-
derclays at five levels. One of the latter has large
stumps of Stigmaria and a thin coaly layer

READIN OL IL) > Ae acnes aatep San sataeacebensaneve Pevavasanene
( Grey shale with nodules of ironstone.

Coal 2 inches.
Grey shale 4 inches.
Coal 3 inches.

Coal-group 8... 4 es shale 1 foot 3 inches.

| Argillaceous shale, ironstone nodules, 4 feet.

DOGS. TOSS oRnageece re BE. SE ene OAR eee eee ee nn ae

Grey argillo-arenaceous underlay, ironstone no-
dules, and Stigmaria.

The roofs of the first and second beds in this group are
among the richest in fossils in the Joggins section. They
have afforded Pecopteris lonchitica, Cyclopteris, Cyperites,
Cordaites borassifolia, Cardiocarpum fluitans, Sigillaria
elegans, Lepidophloios Acadianus, Lepidodendron undulatum,

113

ft. in.

2

30

68

2

0

1

114 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec..20,

Pinnularia, Trigonocarpa, &c.; also Diplostylus Dawsoni*,
Eurypterus, Cythere, Naiadites, and Spirorbis attached to
plants. The lower coal, called locally the ‘‘Queen’s Vein,”
has in its mineral charcoal bast. cells, uniporous, rari-
porous, and multiporous wood-cells, scalariform vessels,
epidermal tissue, and vascular bundles of ferns, also stipes
of ferns and bark of Stgillarza. The mineral charcoal occurs
principally in a thick layer near the bottom of the bed. Its
roof has. trunks of Lepidophloios, Lepidodendron, and Si-
gullaria, fossilized by carbonate of iron. The upper part of
the lowest underclay is dark and carbonaceous, with Stig-
marian rootlets.

i XXII.

- (Grey sandstones, grey and chocolate shales with

ironstone nodules; three underclays and erect
Calamites and Szgillaria in three beds) ............

XXI.

Grey shale and ironstone nodules.
Coal- jrOuE - | Coal and coaly shale 1 foot 3 inches ..............+06-
Argillaceous underclay, Stigmaria.

The roof contains erect Sigidlarie, Stigmaria, Calamites,
and Cordaites. The coaly shale has fern-stipes and Cor-
daites. The coal itself is coarse and shaly, and has a layer
of mineral charcoal containing bast and epidermal tissue.

There are also in the coal remains of Calamites and Cor-’

daites, and fragments, possibly, of insects.

(Grey and reddish shales with nodules of clay-iron-
stone, and grey and reddish sandstone. One un-
derclay supporting a coaly film, and erect trees at
twa tevells): eri fensanges. Sh0k8 held chee Sect eee

Chocolate shale.
Coal and coaly shale 2 inches.
Coal-group 10... 4 Coaly shale 6 inches. 5 : =
| CoQ Aimee ofac0%- «cc ataeui se sabcostacs aye dennastene nee
| Argillo-arenaceous underclay, Stigmaria.

The upper coal contains flattened Sigillarie and Stig-

maria. ‘The lower bed is hard and unequal, with curved
laminee and obscure traces of petioles of ferns. The mineral
charcoal has bast and scalariform tissues.

XX,

(Red aad grey shales and grey sandstones. Erect Ca-
lamites in one bed. Four underclays) ...,........

XIX,
f Chocolate shale. °
Coal-group 11... Coal and coaly shale 8 inches ..............ececeeeen eee
i Argillaceous underclay, Stigmaria.
The roof has Cordaites, Calamites, and rootlets. The coal
contains much mineral charcoal with the structure of dense

_* Salter, Quart. Journ. Geol. Soc. vol. xix. p. 77.

ft, ini

110 O

28 6

78 6

1865, | DAWSON—COAL-FORMATION. 115

aporous bast tissue; it also contains Oyperites and many ft. in.

vascular bundles of ferns.
(Grey sandstones and argillaceous shale. Erect trees

PROSESFO SOV EIS) foinv's nsbacedas ce gh sd nddd sop SOPa TAURI TOR ENE 37
Grey shale.
Coal-group 12... Coal and coaly shale 1 foot ............se:sececseeeeeee ee il
Argillaceous underclay, ironstone, and Stiqmaria.

The roof contains erect Sigillaria and Calamites, also Cor-
daites with Spirorbis attached, and Lepidodendron. The
coal has in one layer much Cordaites, in others it includes
an immense number of specimens of Sporangites papillata ; it
has also bast tissue, epidermal tissue, and discigerous tissue.

(Shale and sandstone, penetrated by Stigmarian root-
lets, and containing in one of the shales Lepido-

dendron, Sigillaria, and Carpolithes) ......0..100008 13
Grey shale.
Coal-eroup 13,,, + Ceal and coaly shale..,,...-..c.soresessrenseenensaceodsece 0
Argillaceous underclay, Stigmaria.

The roof has much Cordaites. The shaly portions of the
coal contain Sigillaria elegans, Alethopteris lonchitica, Cor-
daites borassifolia, Lepidodendron, Diplotegium, Trigono-
carpum, Stigmaria, and Sporangites glabra, also vascular
bundles of ferns and bast tissue.

XVIII.

(Grey and red shales and grey sandstone ; one of the
latter with erect Calamites and Sigillarie. One

TABU CEUINW Docs gts uasniatvaiicia sth wena y eka es stag ava 4 69
| XVII.
Grey shale.
Wam-erang tad.) Opal S inches 5..15...ics.cscseacdeeenddeaeneseensdussGerecnec 0
Argillaceous underclay, Stigmaria.

The roof has Cordaites and many decayed stipes. The
coal has Cordaites and vegetable fragments.

XVI.
(A very thick sandstone with shales. Erect Cala-
mites, footprints of reptiles, and rain-marks)...... 57
xy.

Grey shales with ironstone.

Coal 3 inches.

Coaly shale 2 inches,

Coal 3 inches.

Underclay, Stigmaria, 6 feet.
Coal-group 14... Coaly shale 4 inches.

Underelay, Stigmaria, 1 foot.

Coaly shale 8 inches.

Coal euanelie re is bates ka 8 10

Argillo-arenaceous underclay, Stigmaria, and iron-
{ stone.

On the roof of the upper coal is a fine-ribbed S dette
with Stigmarian roots. In the roof and shaly partings

116 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

are Sigillaria Brownii, S. Schlothetmiana, and other species,
Stigmaria, Lepidodendron, Calamites, Cordaites, Sporangites
glabra, Alethopteris lonchitica, Sphenopteris latifolia, Pinnu-
laria, and Cyperites ; also Cythere, Naiadites, and fragments
of reptilian (?) bones. The coal is pyritous, and exhibits im-
pressions of the bark of Sigillaria; it contains also bast
tissue, scalariform tissue of Sigillaria, and multiporous tissue
of Sigillaria and Calamodendron.

(Sandstone and shale, erect Calamites and Sigillaria
with S¢igmaria. The erect trees contain repti-
lian remains of the genera Dendrerpeton, Hylo-
nomus, and Hylerpeton ; also Pupa vetusta, Xy-
lobius Stgillarie, and remains of insects) .........

Coaly shale.

Coal-group 15... ; Coal. 6 inches .5:i5 sitiewe denis suwiadio vddlecap ea aea eee

Arenaceous underclay, Stigmaria.

The erect trees above mentioned are rooted in the roof of
this coal. It contains Cyperites, Lepidophylla, Trigonocarpa
of 2 species, Sphenophyllum, Alethopteris lonchitica, Cordaites,
and Asterophyllites. There are shells of Spirorbis on some
of the plants. The coal contains layers of bark of Sigillaria
and leaves of Cordaites, and much bast tissue, with scalari-
form, uniporous, and reticulated tissues, probably of Sigil-
laria.

(Sandstones and shales; erect Calamites and Stig-

GHOPTE) Viroe sansient ucavivsceadtags sos Raha ene eee

Grey shale.

Coal-group 15a | Comb AMMCWeS, ce shnsisnneies \oesireee is hobe sale octane eee

Argillaceous underclay, Stigmaria.

The roof contains Calamites, Sigillaria, Alethopteris lon-
chitica, Pinnularia, Lepidodendron, Cyperites, Sporangites,
and Spirorbis. One Srgillaria extends 30 feet without
branching. The roof supports an erect tree. The coal is

filled with flattened stems of Srgillaria lying im different —

directions, also flattened Lepidodendra; and in its mineral
charcoal it has beautiful porous and scalariform tissues,

XIV.

(Grey sandstone and grey and red shales. Many
prostrate trunks of Sigzlaria and Lepidodendron,
one undetclay, and erect trees at one level) .,....

Shale with the aspect of underclay.
ae Coal and coaly shale 6 imehes snweears- ketene
Coal-group 16... Argillo-arenaceous underclay, ironstone, and Stzg-
maria.

This bed was not well exposed, and afforded no fossils.

(Grey sandstone and shale with one underclay)......
Grey shale.
Coal-group 17... 4 Coal and coaly shale 3 inches ...........cececsseseneeees
’ Argillo-arenaceous underclay, Stigmaria.

The roof has vegetable fragments and Oordaites. The

ft. im,

10 0
0 6

21

6

8

GC oq

865. | DAWSON—COAL-FORMATION.

coal is hard and coarse, and contains flattened broad-ribbed
Sigillaria, Cordaites, and vascular bundles of ferns.

(Shale and sandstone, erect trees at one level) ......

XIII.
Grey shale.
Conleemp lS... Coal 8 iMches-..; 4.01.5. csv0ssescdeceasensapotiveesvnseansnes

Argillo-arenaceous underclay.

The roof has an erect Sigillaria. The coal is shaly and
laminated. It contains much Cordaites, also Lepidodendron,
Calamites, and Alethopteris lonchitica. In one layer there
are Naiadites, Spirorbis, and scales of fishes.

(Grey sandstone and shale in several beds, Stig-

NOTA) date 5 stint Nea rlinn d oubpticointiie See nadie Ga esas anys
Argillaceous shale.

Coaly shale 4 feet.

Bituminous limestone 2 feet 6 inches,
(OGRA Shc) Ce ek Se: Se cae ee ae

The roof has Naiadites, scales and teeth of fishes, Cythere,
and Spirorbis. The coal is hard and coarse, with vascular
bundles of ferns and prostrate Sigillarie. —

(Shale and sandstone)... ..cvsvceveussevecnecctcaeyanessr
Coaly shale 1 foot.

Coal-group 20... | Bituminous limestone 1 foot 6 inches.
Coal and clay partings 2 feet 4 inches..............066

Coal-group 19...

The roof has Naiadites, Spirorbis attached to plants, and
small rhombic fish-scales. The coal alternates with lime-
stone at the top, and contains remains of Sigillaria, Sporan-
gites, and vascular bundles of ferns.

(Sandstone, and grey and black shale with coaly
PIERS erm rahe Se intr Se ww setae eee Satdnamine ad uch chiles Saben
Grey shale and calcareo-bituminous shale.
Coal-group 21... gece IMC OS sia apis that caps a ctocte a's souadradlsiag§ ve vas’
Argillaceous underclay, Stigmaria.

The roof has obscure vegetable fragments and Nazadites.
The coal contains vascular bundles of ferns, bast tissue,
uniporous cells, and scalariform and reticulated vessels.

(Grey sandstone and shale. Two underclays).........
Grey shale.

Coal-group 22... Coal and coaly shale 2 inches Roveqenn hl fad
Argillaceous underclay, Stigmaria.

This bed was not well exposed. |

(Sandstone and shale, with one erect tree and two

AVE OR CLAYS) Meee Sova nit we Bs Tuiclom ee ciesieeeinenioRe enty salen vanes
Coaly and grey shale.
Coal and coaly shale 4 inches.
Coal-group 23... 4 Bituminous limestone 4 inches.
|. Coal and. cosy shale: 7 Imehes2).. Jvwen-hpitesseaeorsaves
| Argillo-arenaceous underclay, Stigmaria,

The roof has an erect tree, also Cordaites and Spirorbis.

The shale and bituminous limestone contain Sigillaria and
VOL, XXII,—PART I. K

117

fia ine.

3l 3

4 10

21 0
0 10

20 0

a)

118 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Dec. 20,

Lepidophloios, also many large-furrowed trunks, probably
old Sigillarie or Lepidodendra.
| moe : XII.
_ (Sandstone, shale, and calcareo-bituminous shale with
threecandenc lars ce coset veces <cwitns cermdeane cease
Calcareo-bituminous shale.

Coal-group 24... Coal and coaly shale 1 inch ..........:....060e04 eae
Argillo-arenaceous underclay, Stigmaria.

This bed was not exposed.

(Underclay and shale)......... coshieigeee alleles ae ain

3 Grey shale.
Coal-group 25... Coal and coaly shale 8 incties 2.../, ee
Sm Argillo-arenaceous underclay, Stigmaria.

The roof has Alethopteris lonchitica, Cordaites, and pe-
tioles of ferns. The coal shows bast tissue and remains of
Sigllaria and Calamites.

(Grey sandstone and shale, with erect Stgillarie at
four or five levels, and two Stigmarian under-
C1 S) He sasenrientiene ious meee Waves Soi shay cake gaeee
Grey shale. .
Coal-group 26... 4 Coaly shale 4 inches ...........:..cseeseeneeeeeeeees thbsewd
: _ ss | Argillo-arenaceous underclay, Stégmaria.

This bed was not exposed.

(Shale and sandstone, with Stzgmarid)......0..0.0.006
Grey shale.
Coal-group 27... ; GoGl BS: WGHES v5 0. viv We iyey eb scdes ens bree! Whee donee
Argillo-arenaceous underclay, Stigmaria.

This bed was not well exposed.

(Grey sandstone and shale, with bituminous shale
and limestone, and erect Calamites) ...............
Xi;
( Calcareo-bituminous shale.
| Coal and coaly shale 7 feet.
| Underclay, Stigmaria, 4 feet.
Coal-group 28... Coaly shale 1 foot.
Coal @ CWS x4... ss ge: cu oak A eee een gee eee sane
\ Arenaceous underclay, Sein aree
This group is a series of thin coaly layers and underclays.
The roof has Navadites carbonarius and N. elongatus, also
Cythere and scales of fishes. The coal contains bast tissue
and different kinds of scalariform and epidermal tissues. In
the lower bed is a coaly stump and an irregular layer of
mineral charcoal, arising apparently from the decay of
similar stumps.
(Grey and carbonaceous shale and grey sandstone)...
Underclay, Stigmaria.
Coal and coaly shale 5 feet.
Coal 99. | Underclay 6 feet.
aaa Scan |e coaly shale, and ironstone, 6 feet.

CoOLes: SOO sere eootocat leak mU ERR REEL eee wat ae ek <ieas
Argillaceous underclay, Stigmaria.

dt, itty

iby g

64

12

29

21

0

0

1865. | DAWSON—COAL-FORMATION.

This is a group of unusually thick beds, indicating long
quiescence. The roof includes lamine of coal, some of them
composed of the bark of Stgillaria catenoides, also an erect
Sigillaria rooted in the coal below. The coal and coaly shale
exhibit remains of Sigillaria, Cordaites, Lepidophyllum, and
OCyperites; and one layer has many hard pyritized fragments
of wood. The mineral charcoal has vascular bundles of ferns,
coarse scalariform tissue, and porous tissue. The underclay
rests on a bed with Naiadites.

(Underelay, Stigmaria, and grey and carbonaceous
RWW 253 cows sides setebretee ected eects seers be Nav euperks
Shale and coaly layers.
Coal-group 29a. GEM eon ra cease <2 oRvachys Maes ced ehabeareteheuandses
Argillaceous underclay, Stigmaria.

The roof has obscure fragments of plants and stumps in .

the state of mineral charcoal. The coal shows impressions
of flattened trunks, probably Sigillaric. This coal contains
a great variety of tissues, especially bast and scalariform of
different kinds, and epidermal. My measurements in this
part of the section differ somewhat from those of Sir W. E.
Logan, who, I suppose, had not a good opportunity of ex-
amining the two last coals. The coal 29a is now mined by
an adit from the shore, called the “‘ new mine.”
(Sandstoneand shale. One sandstone has riany large
erect Sigillarig, some of them with rough and
AEE ONO PARK). ccccrsssicpeo taste oMbacriaceogetenheece
-Argillaceous shale and ironstone,
Coal 4 inches.
Underclay, dark-coloured, 2 feet. *
Coal-group 30... a tier eas shale 2 inches.
Coaly shale 2 inches.
Coal Dancy ji.tgsett. bp. sh adapaigateets ty’: piceclaerernses vs
\ Soft argillaceous underclay, Stigmaria.

The roof has bark of Sigillaria preserved in ironstone.
The coal is pyritous, and consists of layers of mineral char-
coal alternating with bright coal; it has obscure impressions
of plants and bast tissue in the mineral charcoal.

XxX.
(Grey shale and sandstone. One underclay, and
erect Calamites and Sigillaria at two levels) ......
f Grey sandstone.
Coal and coaly shale 1 foot.
Underclay, Stigmaria, 1 foot.
|ot-proupdl... Coaly tale 6 ee,
Coal. 2 WRONG Bice goateciwer ces uneven sasieeeen sea ae ose
Argillaceous underclay, Stigmarza.

The roof contains Sigillarie, and the coal has flattened

impressions of the same. This coal is remarkable as having a _

roof of sandstone. Its underclay isalso peculiar. It is about
9 feet in thickness, and contains Stigmaria and nodules of
K 2

119

ft, En.

18 0
4 Q

35 0

19 0O

120 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20

ironstone throughout. It rests on a bituminous limestone
containing Naiadites and scales of fishes, and also large roots
of Stigmaria evidently a situ. This bed gives more colour
to the idea of Stigmaria having grown under water than any
other bed at the Joggins. I believe, however, that it merely
implies the drying-up of a pond or creek into a swamp, sub-
sequently inundated at intervals with muddy water.

(Underclay and bituminous limestone, succeeded by

sandstone and shale) ............0 ersig:nonaasiaite een eeeee
Grey shale.
Coal-group 32...4 Coal and coaly shale 2 feet 4. inches ..... ssp atsel-enis
Argillo-arenaceous underclay, Stigmaria.

This is a series of thin coaly bands alternating with shales.
The roof contains trunks of Sigillaria, Cordaites, Alethopteris,
and Cyperites. The coal has numerous flattened trunks of
Sigillaria.

(Grey and reddish sandstone and shale. Five under-
clays, one with a film of coal and erect Stgillarie
at two levels)

Coaly shale.
Coal-group 33...4 Coal 1 inch....... atin wos Sg alenag skp Ronee cir ee eee
Argillaceous underclay, Stegmaria.

The roof has flattened trunks and vegetable fragments.
The coal is a mere soil, with remains of Sigillaria and Cor-
daites, and vascular bundles of ferns.

(Red and grey sandstone and shale)
Grey shale.

Ce Oe OR eC

@eeceseOOGsoeseotoeeteos

Coal-group 33a.

Coal and coaly and grey shale (underclay).
Argillaceous underclay, Stigmaria.

These layers, though not of sufficient importance to be
measured as coal-bands, are most interesting as furnishing
examples of what may be termed rudimentary coal-beds.
Kach layer is plainly composed of prostrate trunks of Stgz-
laria resting on Stigmarian underclay, and mixed with Cor-
daites, Alethopteris lonchitica, and vascular bundles of ferns.
In one layer is a stump in the state of mineral charcoal.
In another there are coprolites, scales of fishes, Spzrorbis,
and fragments of Crustaceans. In a reddish shale above
these beds there is a patch of grey sandstone interlaced with
Stigmarian roots, as if the sand had been prevented from
drifting away by a tree or stump.

(Reddish and grey sandstones and shales, with three
or more underclays, having their coaly layers
holding Stgillaria. Erect Stgillarie at two levels)

Underelay, with ironstone and Stigmaria.

Coal and coaly shale 2 inches.
Coal-group 34...< Underclay, with ironstone and Stigmaria, 4 feet.
Coal and coaly shale 2 inches ............. veeeeseceenese
Argillo-arenaceous underclay, Stigmaria.

Only obscure vegetable fragments were observed.
(Grey and reddish sandstone and shale, with Stig-

NAME) ic anceseorendeicnieniadt canon aun tnenertnareadearbaaniganiee

5 rman

27 8

149 O

246 0

13 10

1865. ]. DAWSON—COAL-FORMATION. 121

Underclay with Stigmaria. ft. in.
Coal-group 35... 1 Coaly shale 3 inches ........ » sss a tniaPanacuadaeahaltitis jsnbe 03
Red and greenish underclay, a few rootlets.

The coaly shale contains many leaves of Cordaites borassi-
folia.
(Red, grey, and dark shale, sandstone, and bitu-
minous limestone. Three underclays and erect
trees ab one level) s..s.cs<cisascancceosess Suanecucateana 67 9

1X,
( Bituminous limestone.
Coaly shale and coal 3 inches.

Coal-group 36... 4 Reddish shale and ironstone, 2 feet 6 inches.

IG Ge) AMC DES ia con aude oar capiee vee teen Wianadetaeseeaaiccs sie 3 0

\ Argillaceous underclay, Stigmaria.

The roof has Stigmaria in situ, and has been a soil or

underclay. It also contains Cythere, fish-scales, coprolites,
and Spirorbis. In the upper coaly shale are prostrate car-
bonized trunks. |

(Reddish and grey shale, sandstone, and bituminous
MMSKLONG) 5... Fcek eee sees ded eteva mentee kaos eaevate ese 21 6

Bituminous limestone and shale.

on 4 inches.
Underclay 1 foot 6 inches.

| Coal 6 inches.

Coal-group 37... 4 Underclay 1 foot.

Bituminous limestone 3 inches.
Shale 3 inches.
Gearlog heen Seva ten leas eget doves oslea stays 3 11
Underclay with Stigmaria.

The roof has Stigmaria, also fish-scales, Natadites, and
Cythere. The shales are pyritized. The coal shows only
obscure fragments of plants; but Szgillarie in the state of
ironstone occur in some of the clays.

VIII.

(Red and grey sandstone and shale. Two under-
clays. Many shells of Pupa vetusta occur in one
of these, about 12 feet below the last coal)......... 83 0

VII.

Calcareo-bituminous shale,
Coal 1 inch.
Coal-group 38... { Bituminous limestone 6 inphex,
| Coal 2 inches.
Underclay passing into chocolate shale, Stigmaria.
The bituminous limestone and shale contain Cythere,
Naiadites elongatus and N. carbonarius, coprolites, Spirorbis,
and Stigmaria. The lower coal has Stgillaria elegans, S.
scutellata (?), S. Brown, Alethopteris lonchitica, Cordartes
borassifolia, and vascular bundles of ferns.

(Red and grey shales and sandstones, and one grey
limestone with Cythere. One underclay. Many
drift trunks, among which are Sigillaria and
LCpPUdoPhlotOs)), | wuss sivsieinnsies Oo Ceske waa edoes 123 6

122 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 2.

Vv.

Red and grey shale, with ironstone,

COs Finely (5) aa pee renee eee a res nes foe ce

-Grey underclay, with Stigmaria, resting on bitu-
minous limestone, with Stigmaria and Cythere.

Coal-group 39...

This thin coal consists of a layer of flattened trunks, pro-
bably of Sigidlaria, with a quantity of mineral charcoal.

IV.

(Red and grey shales. One bed with erect Calamites,
another with erect Sigillarid) .......sccerceeveeneeees

III.

Grey shale and ironstone.
Bituminous limestone and shale, with coaly films,
7 inches.

Underclay 1 foot.

Coal 1 inch.

Coaly shale 3 inches.
_Underclay 1 foot.

Bituminous limestone 6 inches.

Coal and. coaly shale 2 inches suissnesscauvevsasencssavie
Argillaceous underclay, ironstone, and Stigmaria.

Coal-group 40...

The bituminous limestone and shale have WNaradites,
Cythere, Sprrorbis, scales of fishes, and coprolites, and a large
spine of Gyracanthus, also roots of Stigmaria. The upper
underclay holds carbonized erect trunks. The lower coal has
vascular bundles of ferns and Cordaites. The roof supports
erect stumps.

(Underclay with ironstone nodules) ...............00008
Underclay as above.
Coal-group 41... Calcareo-bituminous shale and films of coa/ .........
Argillaceous underclay, St¢gmaria.

The bituminous limestone has Naiadites carbonarius,
Cythere, coprolites, and Spirorbis. The roof has prostrate
Sigillarie converted into coaly layers. The underclay has
distinct stumps of Stagmaria. |

(Shales with Stigmaria and ironstone, sandstones,
bituminous limestone, and carbonaceous shale at
BOGEOM ) ices snes akieste swe taka g aRtedaneRaRReeE ee ae EEE
( Bituminous limestone.
Coal 3 inches.
Shale 1 foot.
Coal-group a Coal 1 foot.
Underclay, Stigmaria, 1 foot.
Coal 2 inches .........0.+ ei Blas datecannnjos bale Ba RgeeMene
\ Dark argillaceous underclay, Stigmaria.

The roof contains Naiadites, Cythere, and coprolites. The
coal is coarse, pyritous, and shaly, and has bark of Sigillaria,
Calamites, and vascular bundles of ferns. It seems to be the
edge of a bed, as it thins rapidly in the direction of the bank,

or to the east.

65 4

14 4

“ch 9 Si a DAWSON—COAL-FORMATION. | 128

TE. fait ffi; 1.

(Reddish shale and sandstone with one underclay 30 0
Reddish underclay with Stigmaria.

Coal-aroapas,,.4 Coaly shalo | inch .,.4...,sscecsecoprenannecrrsnscgeatateres ae |
Reddish underclay, Stigmaria. .

This bed diminishes to a mere film towards the bank.

I. i

(Reddish, grey, and dark shales and sandstone, Stigq-
maria in some beds, and erect Sigillarie and
Calamites at, On© level): iss és sacievdsoneseres«sereree-neg OB

- ( Grey shale with ironstone.
Bituminous limestone and shale with ironstone, 10ft. 1in.
Coal 4 inch.
Bituminous limestone, Stigmaria, 4 inch.
Coal 5 inches.
Coal-group 44... 4 Bituminous limestone, Stigmaria, 2 inches.
Coal 1 inch.
Bituminous limestone, Stigmaria, 2 inches.
ER ae et cata dec dha dels dy isk EI i RA Aas Vitis vvses ll 0%
\ Argillo-arenaceous underclay, traces of rootlets.

The bituminous limestone has scales of fishes, Spirorbis,
and Cythere. The coal has Cordaites and vascular bundles

of ferns.
(Red and grey sandstone and shale. One underclay,
and erect Calamites at one level) ..........:.sesseeees 98 6
( Reddish shale.
-Carbonaceous shale, 10 inches.
Coaly matter 4 inch.
Hard underclay, Stigmaria, 2 feet.
Coaly matter 4 inch.
Underclay, Stigmaria, 7 feet.
Social eR HING HGH Acrte.anp snenutdcsenag sad tcd dee piairsnsecves- 10 2
\ Arenaceous underclay, Stigmaria.

In the roof of the lower coal is an erect tree. The coal has
vascular bundles of ferns, remains of fern-leaves, and bast
tissue. The underclay has many coaly films, apparently

flattened bark of trees.
Reddish and grey sandstone and shale ....,... gear 5 6

Coal-group 45...4
|

Total thickness of Division 4, according to Logan’s measurements...... 2539 1

e. Division 5.—This consists of reddish shales and red and grey
sandstones. It contains no coal, and is poor in fossils, only a few
drifted trunks appearing in the section. It corresponds to the upper
part of the Millstone-grit series. Its thickness, according to the
_ measurements of Sir William E. Logan, is 2082 feet.

f. Dwision 6.—This may be regarded as the middle of the Muill-
stone-grit series. It constitutes a sort of false coal-formation, sepa-
rated from the Middle Coal-formation by the barren beds of Division 5.
It contains nine small or rudimentary coal-beds, which, however, are
not well seen in the section, and have afforded few facts of interest.
It has many thick and coarse sandstones and much red shale, with
comparatively few dark-coloured beds. Its total thickness is stated
by Sir W. E. Logan at 3240 feet.

124 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

Though this group contains little coal, it is to be observed that it
has many underclays, indicating soils which supported forests of
Sigillaria, and that erect Sigillarice occur very near the base of the
division. The absence of important beds of coal is therefore due to
the local physical conditions, and not to the want of the ed

vegetation.

(Sandstones and il with many drifted trunks of i

DAdORGQlON) is siasiasetee ae toed ain va kedsgdos Sane daevemeatonenee
Blackish grey shale.
Calcareous shale 1 foot.
Coal-group 1 ...< Black shaie 3 feet.

Coaly shale 2) ime Wes tes eceennot. vane i sea aioe setae -

Argillo-arenaceous underclay, Stigmaria.
(Red and grey sandstone and shale and concretionary
limestone," trunks of Dadoxylon and other trees.
One uniderclaiy)).2..0c:s00.s.dhetedsld. dee ee
Grey shale.
Coal-group 2... Cony Shale sl (Cl sit siisie ae ca edne tye Meee ok eee
Reddish and grey underclay, Stigmarza.

(Series of underclays with Stigmaria. 'The beds are -

reddish or grey, and arenaceous)............seseeeee
( Reddish shale.
Coaly shale 1 inch.
Greenish shale 6 inches.
Coaly shale \ inch.
Coal-group 3...4 Greenish shale 2 feet 6 inches.
Coaly shale 3 inches.
Greenish shale | inch. é
Coal and coaly shale 3 inches ..........0:secsrssteeveoen
Argillo-arenaceous underclay, Stigmaria.

The coal contains bast tissue and reticulated, porous, and
scalariform tissues of Sigillaria and Calamodendron.:

(Series of underclays as before).......<.«0.0-sesaseeeeeee
' Underclay, Stigmaria.
Coal-group 4... Coal and coaly shale 3 inches ........:.26--seosmswense
Argillo-arenaceous underclay, Stigmaria.

(Series of underelays as before) 2............¢os«seseseemene
Grey shale. :
Coal-group 5... Coaly, matter > Wich... je cescsccavaden Papbeboccon Gc wae
Greenish underclay, Stigmaria.

(Underelay and sandstone, the latter with an erect
SEGTLAPUA) oo... Seas Sunssndelele «Saeko ais eeeeee ee ema
Sandstone (erect Szgil/aria as above),
Coal-group 6... Coaly shale 3 inches. ....,.:.....s:.+0sJcecuaes: seen
Argillo-arenaceous underclay, Stigmarza.

(Fifteen feet of underclay, under which a thick sand-
stone with great quantities of drifted trunks of Da-
doxylon and Sigillaria. Below this alternations
of grey and red sandstone and shale) .........0.....

( Grey sandstone.

Bituminous limestone 3 inches.

Grey shale 3 feet.

Grey limestone 2 inches.

Coal-group 7 ...4 Coaly shale 6 inches.

Bituminous limestone 3 inches.

Coaly shale 1 foot. :

Cog! WAmeln acess cap ase es oe Le eveeteons

\ Argillo- arenaceous under clay, Stigmaria.

in.

539 7

160. 4 -

12

10 0

210 10

1865. ] | DAWSON—COAL~FORMATION. 125

The lower bituminous limestone contains Natadites ovalis, ft. in.
Cythere, and scales of Lepidoid fishes. The lower coal has
much Cyperites and bark of Sigillaria, also bast tissue in
mineral charcoal.

(Thick beds of grey sandstone and grey shale, with
drifted trunks of Dadoxydon, Sigitlaria, and Ca-

lamites, and leaves of Cordattes) ......4. Sagcngce gta 5382 0
i Grey shale.
rR sn COU) © INCOM oneie secs nner sesdnav coming sOddadwabalees weed nee 0 4
| Argillo-arenaceous underclay, Stigmaria.

This coal is laminated, the laminz being bark of Szgil-
larie. The underclay is very rich in Stigmaria.

(Grey sandstone with grey and red shale. Many
drifted trunks of Stgzllaria and Calamites, and an
erect Sigillaria in the lowest bed of sandstone)... 1224 0
Grey shale.
Coaly matter and carbonaceous shale .........s00.0. 6 Or?
Argillo-arenaceous underclay, S¢igmaria, and iron-
stone.

Coal-group 9...

(Grey and red sandstone and shale and calcareous
bands, some of them bituminous. Near the
middle a thick band of laminated black shale with
Naiadites levis, Cyperites, and Lepidostrobus.

Drifted Calamites in the sandstones) .........+. 496 4

ore etmckness, ACCOFdING to Logan «2.0... 0..cecacesedsvecsoscsevasessseveses O24 Q

g. Division 7.—This division consists principally of red and choco-
late shales with red and grey sandstone, arenaceous conglomerates,
and thin beds of concretionary limestone. It may be regarded as the
base of the Millstone-grit formation. Its thickness is stated by Sir
W. E. Logan at 650 feet.

' No fossils, other than carbonized fragments of plants, have been
found in this division. |

h. Division 8.—This division consists of reddish shales with green-
ish and red sandstone, grey shale, grey compact limestone, and gyp-
sum. It may be regarded as the upper part of the Lower Carboniferous
formation ; and almost immediately under its lowest beds there are
- marine limestones with Productus cora and other characteristic Lower
Carboniferous fossils.

Only fragments of plants, often replaced by sulphuret of copper,
have been found in this division. Its thickness is stated by Logan
at 1658 feet.

“$ TY. Remarxs on THE ANIMALS AND PLANTs WHOSE REMAINS occUR
IN THE COAL.

1. Introduction.—Under this heading I shall, in the first place,
present a tabular view of the relative frequency of occurrence of the
several genera in the beds of coal and their roof-shales, without
reckoning the almost invariable occurrence of Siigmaria in the under-
clays, which is of course to be taken as an indication of the existence
of Sigillarioid trees in connexion with the growth of the coal.

126 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 20, .

The number of coals reckoned may vary according to the manner
in which the several layers are grouped; but as arranged in the
above sectional list it amounts to eighty-onein all. Of these, 23 are
found in Division 3 of Logan’s section, being the upper member of
the Middle Coal-formation ; 49 are found in Division 4 of Logan’s
section, being the lower member of the Middle Coal-formation; 9
occur in Division 6 of Logan’s section, or in the equivalent of the
Millstone-grit. In the latter group few of the coals were suffi-
ciently well exposed to enable a satistactory examination to be made.
I have grouped the remains under three heads—External Forms of
Plants, Microscopic Structure of Plants, and Animal Remains—and
have arranged the forms under each in the order of their relative
frequency of occurrence.

Table showing the Relatiwe Frequency of Occurrence of Genera of
Plants and Animals in the Coals of the South Joggins.

Division 3.| Division 4.| Division 6.| Total.

ighiaras @. Eioeet Fe 23 coals. | 49 coals. | 9 coals. |81 coals.
Plants
Sioillariaatwapcanaeees occurs in 13 34 7d 49
Cordaites =... ssssec8 a 15 26 ay 41
Filices (mostly Aletho-

pteris lonchitica) on i = a 2 23
Lepidodendron and

Lepidophloios ... i } : = 16
Calanaities: : ccs <neeese i 4 12 16
Carpolites, &c. ...... " 2 a : Ey
Asterophyllites ...... * if 2 3
Calamodendron ...... ey ies l Svan, We ps

Structures.
ee eae 22 | 80
Bast tissue (Sigtllaria) _,, 2 16 D, 20
Epidermal tissue

( Cordaites, &c.) ... - \ 6 6 12
Scalariform (Szgit.,

Stig., Lepidod., &e.) _,, i l 9 1 Il
Discigerous (Szgzllaria

and Dadoxylon, &e.) ,, \ : 8 1 10
Reticulated ( Calamo- ae: By 1 3

dendron, Ferns, &c.) __,, | ie
Animals.
Fishes (Pale@oniscus,

Rhizodus, &e.) ... ie } U 16 1 18
Naiadites (Anthra-

COMYA, KC.) ....0.+- M } 16 1 17
Spirorbis carbonarius _,, i 16 my 16
CY GRONE catamanracieoctes 3 a lo 1 14
Insects{7) 0.2... p as 3 on 3
Reptiles (Dendrer- Jaa 1

peton, &C.) ......06. : f oe 1
Pupa vetusta and Xylo- 1

bius sigillari@....... da cg 1

1865. | DAWSON—COAL-FORMATION, 127

It will be observed that, whether we regard the external forms or
the internal structures preserved, the predominant plants are Sigil-
laria, Cordaites, and Ferns, with Lepidodendron and Calamites. The

‘substance of the coal itself, so far as its structure is preserved,

may be said to be principally composed of bark of Stgillaria and
leaves and stems of ferns and Cordaites. In regard to the propor-
tions in different parts of the series, little difference exists, except
that Cordaites and Calamites are rather more abundant in the upper
coals, and Lepidodendron in the lower, while the middle of the series
is the headquarters of Sigillaria and ferns. Remains of aquatic
animals occur in connexion with a large proportion of the coals, more
especially in the middle of the series. This may be explained in
connexion with the theory of growth of the coal in situ by the follow-
ing considerations :—(1) It was necessary to the preservation of the
vegetable matter composing a bed of coal that it should be sub-
merged and covered with sediment. (2) On the submergence of a
swamp covered with standing trees and other vegetation, these would
prevent the. passage of strong currents carrying coarse detritus, and
the area would be covered with fine sediment deposited in still water
and under conditions favourable to certain kinds of aquatic animals.
(3) When the currents carrying detritus were sufficiently powerful
to uproot and sweep away the forests and the brakes of Calamites, they
would also remove or disturb the vegetable soil. It follows that we
should expect the more important coals to be covered with fine sedi-
ment containing animal as well as vegetable remains, and that beds
roofed with sandstone or coarse shale must either have been of small
area or sparsely covered with trees at the time of their submergence.
This accounts for the otherwise anomalous circumstance that the
evidences of aqueous conditions in association with the coal are pro-
portionally more abundant in the middle than in the upper part of
the Coal-measures. We may now proceed to consider the genera of
plants and animals separately, in their relation to the growth of coal.

2. Coniferous Trees.—Four species of coniferous trees, referable to
the genus Dadowylon, have been found in the Coal-formation of Nova
Scotia. They are known to me only by the microscopic structure of
their wood ; but on the evidence afforded by this I have named and de-
scribed them as new species*. One of them, D. antiquius, 1s closely
allied to D. Witham of Great Britain, and, like that species, belongs
to the Lower Carboniferous Coal-measures. Its structure is of
that character for which Brongniart proposed the generic name
*« Paleowylon.” It has not yet been found at the Joggins. Another
species, D. Acadianwm, is found abundantly at the Joggins in the
condition of drifted trunks imbedded in the sandstone of the lower
part of the Coal-formation and the upper part of the Millstone-grit
series, The third species, D. materiariwm, is very near to D. Brand-
lingu of Great Britain, and may possibly be only a variety. It is
especially abundant in the sandstone of the Upper Coal-formation, in

* Descriptions referred to here and in subsequent pages will be found in

* Synopsis of the Flora of the Carboniferous Period,” Can. Nat. vol. viii., and in
the Appendix.

128 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

which vast numbers of drifted trunks of this species occur in some
places. ‘The fourth species, D. annulatum, presents a very peculiar
structure, probably of generic value, It has alternate concentric rings
of discigerous woody tissue, of the character of that of Dadoawylon, and
of. compact structureless coal, which either represents layers of very
dense wood or, more likely, of corky cellular tissue. In the latter
case the structure would have affinities with that of certain Gnetaccce
and of Cycads.

Though coniferous trees usually occur as decorticated and pres-
trate trunks, I have recorded the occurrence of one erect specimen,
in a sandstone a little above the “ Main Coal,” at the Joggins. It
probably belonged to the species last named. ‘Tissues of coniferous
trees are very rare in the coal itself. Most of the discigerous tissues
found in the coal belong to Sigillaria and Calamodendron. From the
abundance of coniferous trees in sandstones above and below the coal,
and their comparative absence in the coal and coal-shales, it may be
inferred that these trees belonged rather to the uplands than to the
coal-swamps; and the great durability and small specific gravity of
coniferous wood would allow it to be drifted, either by rivers or ocean-
currents, to very great distances. I am not aware that the fruits of
pine trees occur at the Joggins, unless some of the Trigonocarpa are
of this character. Nor has any foliage of these trees been found ;
but at Tatmagonche, in the continuation of the Upper Coal-formation,
there are leafy branchlets which I have named Araucarites gracils,
and which may possibly have belonged to Dadowylon materiarvum.

The casts of pith-cylinders known as Sternbergie are abundant
in some of the sandstones, especially in the Upper Coal-formaticn.
I have shown that in Nova Scotia, as in England, some of thesg sin-
gular casts belong to Dadowylon*; but as the pith-cylinder of Stgil-
laria and of Lepidophloios was of a similar character, those which are
destitute of woody investment cannot be determined with certainty,
though in general the transverse markings are more distant in the
Sternbergre of Sigillarva and Lepidophloios than in those of Dado-
vylon.

5 Plate V., and in Plate VI. fig. 14, I have given illustrations of
the coniferous ‘plants above referred to.

3. Sigilarie.—I have catalogued or described no less than twenty-
one species belonging to this family, from the Coal-measures of Nova
Scotia. They may be arranged under the following provisional
genera :—

(1.) Favutarz, Sternberg .... Sigillaria elegans, Brongn.
tessellata, Brongn.
Bretonensis, Dawson.
scutellata, Brongn.
Schlotheimiana, Brongn.
Saullu, Brongn.
Dournaisi, Brongn.
Knorrii, Brongn.

(2.) Ruyripoteris, Sternberg ..

* Proceedings of the American Association, 1837, Canadian Naturalist, vol. 11.
Paper on Structures of Coal, Quart. Journ. Geol. Soc. 1860.

1865. | DAWSON—COAL-FORMATION, 129

(2.) Rayripotepis (continued) _—Sigillaria pachyderma, Brongn.
flexuosa, L. & H.?

elongata, Brongn.

(3.) SrarztaRra, Brongn....... reniformis, Brongn.
Brownii, Dawson.
levigata, Brongn.
planicosta, Dawson.
catenoides, Dawson.
striata, Dawson.

—— eminens, Dawson.

(4.) Crarurarta, Brongn. .... —— Menardi, Brongn.

(5.) Leroprrma, Goldenb. .... ——— Sydnensis, Dawson.

(Asolanus, Wood).
(6.) SyrincopenDRON, Sternd... —— organum, L. & H.

_ Of these, seven are probably new species, and the remainder can be
identified with reasonable certainty with European species. The
differences in the markings in different parts of the same tree are,
however, so great, that I regard the greater part of the recognized
species of Sigillaric as merely provisional. Even the generic limits
may be overpassed when species are determined from hand speci-
mens. <A fragment of the base of an old trunk of Sigiilaria proper
would necessarily be placed in the genus Leioderma, and a young
branch of Favularia has all the characters of the genus Clathraria.
It is, however, absolutely necessary to make some attempt at generic
distinction among the diverse forms included in the genus Stgillaria ;
otherwise it will be impossible to reconcile the conflicting statements
of anthors as to the dimensions, habit of growth, foliage, roots, and
fructification of these singular plants ;—such statements usually ap-
plying to one or more of the subordinate generic types. I shall
therefore notice separately, and with especial reference to their
function in the production of coal, the several generic or subgeneric
forms, beginning with that which I regard as the most important—
namely, Sigilaria proper, of which, in Nova Scotia, I regard the
species which I have named S. Brownz (figs. 15 to 20, Pl. VI.) as
the type. Other species are represented in figs. 21 to 28.

In the restricted; genus Sigillarza the ribs are strongly developed,
except at the base of the stem; they are usually much broader than
the oval or elliptical tripunctate areoles, and are striated longitu-
dinally. The woody axis has both discigerous and scalariform tissues,
arranged in wedges, with medullary rays as in exogens*; the
pith is transversely partitioned in themanner of Sternbergia; and
the inner bark contains great quantities of long and apparently very
durable fibres, which I have, in my descriptions of the structures in
in the coal, named “ bast tissue.” The outer bark was usually thick,
of dense and almost indestructible celiular tissue. The trunk when
old lost its regular ribs and scars, owing to expansion, and became
furrowed like that of an old exogenous tree. The roots were Stig-
marie of the type of the ordinary NS. ficoides. I have not seen the

* Quart. Journ. Geol. Soc., paper on Structures of Coal.

130 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

leaves or fruits attached ; but, from the associations observed, I believe
that the former were long, narrow, rigid, and two- or three-nerved
(Cyperites), and that the latter were Trigonocarpa, borne in racemes
on the upper part of the stem. These trees attained to a great size.
I have seen one trunk four feet in diameter, and specimens of two
feet or more in diameter are common: some of these trunks have been
traced for thirty or forty feet without branching. ‘The greater
number of the erect stumps preserved at the Joggins appear to belong
to this genus, which also seems to have contributed very largely to
the formation of coal. Judging from the paucity of their foliage, the
density of their tissues, and the strong structural resemblance of
their stems and roots to those of Cycads, I believe that their rate
of growth must have been very slow.

The genus Rhytidolepis, in which the areoles are large, hexagonal,
and tripunctate, and the ribs narrow and often transversely striate,
ranks as a coal-producer next to Sigillaria proper, and is equally
abundant in the Coal-measures. These trees seem to have been of
smaller size and feebler structure than the last mentioned, and are
less frequently found in the erect position; but they are very abun-
dant on the roofs of the coal-beds. Judging from such specimens
as I have seen, their roots were less distinctly Stigmarioid than in the ~
last genus, though this appearance may arise from difference of pre-
servation. Their leaves were of the same type’as in the last genus ;
and their stems bear rings of irregular scars, which may mark stages
of growth, or the production of slender racemes of fruit in a verti-
cillate manner. The woody axis of the stems of this genus was com-
posed of scalariform and coarsely porous tissues, much like those of
modern Cycads. I figure, as an illustration of the genus, a fragment
of S. scutellata showing one of the belts of abnormal scars. |

The genus Favularia is represented in Nova Scotia principally by
the typical species S. elegans of Brongniart. The admirable investiga-
tions of the structure of the stem of this species by Brongniart, with
the further illustrations given by Corda, Hooker, and Goldenberg, still
afford the best general views of the structure of Sigillarie which
we possess*. Itis to be observed, however, that Brongniart’s speci-
men was a young stem or a branch, and that it affords a very imper-
fect idea of the development of discigerous and bast tissues in the
full-grown stems of Sigillaria proper. ‘The trees of this genus ap-
pear to have been of small growth; and they branched in the manner
of Lepidodendron, the smaller branches being quite destitute of ribs,
and with the areoles elliptical and spirally disposed. The stems show
joints or rings of peculiar scars at intervals, as in the last genus.
The leaves differ from those of the other genera, being broad and with
numerous slender parallel veins, almost in the manner of Cordaites.
(Figs. 26 and 27, Plate VII.)

The genus Clathraria is evidently closely allied to the above,
and is possibly founded on branches of trees of the genus Favularia.
It is a rare form in Nova Scotia.

* See also Binney “ On some Fossil Plants showing Structure, from the Lower
Coal—measures of Lancashire,” Quart. Journ, Geol. Soe, vol, xviii, p. 106.—Eprr.

1865.] ' DAWSON—COAL-FORMATION. 131

é Of the genus Leioderma or Asolanus I know but one species, inde-
pendently of those specimens of old trunks of the ordinary Srgillaria
in which the ribs have disappeared. My species, S. Sydnensis, is
founded on specimens collected by Mr. Brown at Sydney, Cape
Breton, which are especially remarkable for the curious modification
which they present of the Stigmarian root. The specimens described
by Mr. Brown under the name of S. alternans*, and which have
been copied by Geinitz and Goldenberg, belong, I believe, to this
species. (Fig. 28, Plate VII.)

On the genus Syringodendron of Sternberg I have no observations
to make. I have seen only fragments of stems ; and these seem to be
very rare.

I include under Sigillarie the remarkable fossils known as Stig-
maria, being fully convinced that all the varieties of these plants
known to me are merely roots of Sigillaria; I have verified this fact
in a great many instances, in addition to those so well described by
Mr. Binney and Mr. Brown. The different varieties or species of
Stagmaria are no doubt characteristic of different species of Sigillarza,
though in very few cases has it proved possible to ascertain the va-
rieties proper to the particular species of stem... The old view, that
the Stigmarie were independent aquatic plants, still apparently
maintained by Goldenberg and some other paleobotanists, evidently
proceeds from imperfect information. Independently of their ascer-
tained connexion with Stgillaria, the organs attached to the branches
are not leaves, but rootlets. This was made evident long ago by the
microscopic sections published by Goeppert, and I have ascertained
that the structure is quite similar to that of the thick fleshy rootlets
of Cycas. The lumps or tubercles on these roots have been mistaken
for fructification ; and the rounded tops of stumps, truncated by the
falling in of the bark or the compression of the empty shell left by
the decay of the wood, have been mistaken for the natural termina-
tion of the stem}. The only question remaining in regard to these
organs is that of their precise morphological place. Their large pith
and regular areoles render them unlike true roots; and hence
Lesquereux has proposed to regard them as rhizomes. But they cer-
tainly radiate from a central stem, and are not known to produce
any true buds or secondary stems. In short, while their function is
that of roots, they may be regarded, in a morphological point of view,
as a peculiar sort of underground branches. ‘They all ramify very
regularly in a dichotomous manner, and, as Mr. Brown has shown, in
some species at least, give off conical tap-roots from their underside.

In all the Stigmarie exhibiting structure which I have examined,
the axis exhibits only scalariform vessels. Corda, however, figures a
Species with wood-cells, or vessels with numerous pores, quite like those
found in the stems of Sigillaria proper ; and, as Hooker has pointed
out, the arrangement of the tissues in St¢gmaria is similar to that in

* Quart. Journ. Geol. Soe. vol. v. p. 354 e¢ seg.

t For examples of the manner in which a natural termination may be simu-
lated by the collapse of bark or by constriction owing to lateral pressure, see
my papers, Quart. Journ. Geol. Soc. vol. x. p. 35, and vol. vii. p. 194.

132 PROCEEDINGS OF THE GEOLOGICAL society. _— [ Dec. 20,

Sigillaria. After making due allowance for differences of preserva-
tion, I have been able to recognize eleven species or forms of Siig-
maria in Nova Scotia, corresponding, as I believe, to as many species
of Sigillaria*. At the Joggins, Stagmarice are more abundant than
any other fossil plants. This arises from their preservation in the
numerous fossil soils or Stgmaria underclays. Their bark, and
mineral charcoal derived from their axes, also abound throughout
the thickness of the coal-beds, indicating the continued growth of
Sigillaria in the accumulation of the coal. (Figs. 83 to 87 Pl. XII.)

Our knowledge of the fructification of Sigzllarza is as yet of a very
uncertain character. JI am aware that Goldenberg has assigned to
these plants leafy strobiles containing spore-capsules: but I do not’
think the evidence which he adduces conclusive as to their connexion
with Sigillaria; and the organs themselves are so precisely similar to
the strobiles of Lepidophlovos, that I suspect they must belong to that
or some allied genus. The leaves, also, with which they are associated
in one of Goldenberg’s figures seem more like those of Lepidophloios
than those of Szgillaria. If, however, these are really the organs of
fructification of any species of Stgillaria, I think it will be found that
we have included in this genus, as in the old genus Calamites, two di-
stinct groups of plants, one cryptogamous, and the other phenogamous,
or else that male strobiles bearing pollen have been mistaken for spore-
bearing organs.

I cannot pretend that I have found the fruit of Sigillarta attached
to the parent stem ; but I think that a reasonable probability can be
established that some at least of the fruits included, somewhat vaguely,
by authors under the names of Trigonocarpum and Rhabdocarpus
were really fruits of Stgillaria. These fruits are excessively abundant
and of many species, and they occur not only in the sandstones but
in the fine shales and coals and in the interior of erect trees, showing
that they were produced in the coal-swamps. The structures of these
fruits show that they are pheenogamous and probably gymnospermous.
Now the only plants known to us in the coal-formation, whose struc-
tures entitle them to this rank, are the Conifers, Sigillarie, and Cala-
modendra, All the others were in structure allied to cryptogams,
and the fructification of most of them is known. But the Conifers
were too infrequent in the Carboniferous swamps to have afforded
numerous species of Carpolites; and, as I shall presently show, the
Calamodendra were very closely allied to Sigillarie, if not members
of that family. Unless, therefore, these fruits belonged to Sigillaria,
they must have been produced by some other trees of the coal-swamps,
which, though very abundant and of numerous species, are as yet quite
unknown to us. Some of the Trigonocarpa have been claimed for
Conifers, and their resemblance to the fruits of Salisburya gives
countenance to this claim; but the Conifers of the Coal-period are
much too few to afford more than a fraction of the species. One species
of Rhabdocarpus has been attributed by Geinitz to the genus Vaggera-
thia ; but the leaves which he assigns to it are very like those of
Sigillaria elegans, and may belong to some allied species. With

* See Appendix.

1865. | DAWSON—COAL-FORMATION. 133

regard to the mode of attachment of these fruits, I have shown that one
species, Trigonocarpum racemosum of the Devonian strata*, was borne
on a rhachis in the manner of a loose spike, and I am convinced that
some of the groups of inflorescence named Antholithes are simply young
Lthabdocarpi or Trigonocarpa borne in a pinnate manner on a broad
rhachis and subtended by afew scales. Such spikes may be regarded
as corresponding to a leaf with fruits borne on the edges, in the
manner of the female flower of Cycas; and I believe with Goldenberg
that these were borne in verticils at intervals on the stem. In this
case it is possible that the strobiles described by that author may be
. male organs of fructification containing, not spores, but pollen. In
conclusion, I would observe that I would not doubt the possibility that
some of the fruits known as Cardiocarpa may have belonged to
Sigillarioid trees. I am aware that some so-called Cardiocarpa are
spore-cases of Lepidodendron ; but there are others which are mani-
festly winged nutlets allied to Zrigonocarpum, and which must have
belonged to phenogams. It would perhaps be unwise to insist
very strongly on deductions from what may be called circumstan-
tial evidence, as to the nature of the fruit of Sigzllaria; but the
indications pointing to the conclusions above stated are so numerous
that I have much confidence that they will be vindicated by com-
plete specimens, should these be obtained. (Figs. 29 and 30, Pl. VIL.,
and figs. 69 to 79, Pl. XII.)

All of the Joggins coals, except a few shaly beds, afford unequivo-
eal evidence of Stigmaria in their underclays; and it was obviously
the normal mode of growth of a coal-bed, that, a more or less damp
soil being provided, a forest of Sigillaria should overspread this, and
that the Stigmarian roots, the trunks of fallen Sigillarie, their leaves
and fruits, and the smaller plants which grew in their shade, should
accumulate in a bed of vegetable matter to be subsequently converted
into coal—the bark of Sigillaria and allied plants affording “ bright
coal,” the wood and bast tissues mineral charcoal, and the herbaceous
matter and mould dull coal. The evidence of this afforded by micro-
scopic structure I have endeavoured to illustrate in a former paper’.

The process did not commence, as some have supposed, by the
growth of Stigmaria in ponds or lakes. It was indeed precisely the

reverse of this, the Srgillaria growing in a soil more or less swamp.
but not submerged, and the formation of coal being at last arrested
by submergence. I infer this from the circumstance that remains
of Cyprids, Fishes, and other aquatic animals are rarely found in the
- underclays and lower parts of the coal-beds, but very frequently in
the roofs, while it is not unusual to find mineral charcoal more
abundant in the lower layers of the coal. For the formation of a
bed of coal, the sinking and subsequent burial of an area previously
dry seems to have been required. There are a few cases at the
Joggins where Calamites and even Sigiilarie seem to have grown on
areas liable to frequent inundation; but in these cases coal did not
-accumulate. The non-laminated, slickensided and bleached condition
of most of the underclays indicates soils of considerable permanence.
* “ Flora of the Devonian Period,” Quart. Journ. Geol. Soe. vol. vill. p. 324.

+ “On the Structures in Coal,” Quart, Journ, Geol. Soc. 1859,
VOL. XXII.——-PART I. L

134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

In regard to beds destitute of Stigmarian underclays, the very
few cases of this kind apply only to shaly coals filled with drifted
leaves, or to accumulations of vegetable mud capable of conversion
into impure coal. The origin of these beds is the same with that of
the carbonaceous shales and bituminous limestones already referred
to. It will be observed in the section that in a few cases such beds
have become sufficiently dry to constitute underclays, and that con-
ditions of this kind have sometimes alternated with those favourable
to the formation of true coal.

There are some beds at the Joggins, holding erect trees i situ,
which show that Szgidlariw sometimes grew singly or in scattered
clumps, either alone or amidst brakes of Calamites. In other in-
stances they must have grown close together, and with a dense un-
dergrowth of ferns and Cordaites, forming an almost impenetrable
mass of vegetation.

From the structure of Sigillarie I infer that, like Cycads, they ac-
cumulated large quantities of starch, to be expended at intervals in
more rapid growth, or in the production of abundant fructification.
I adhere to the belief expressed in previous papers that Brongniart
is correct in regarding the Sigillariw as botanically allied to the
Cycadacece, and I have recently more fully satisfied myself on this
point. by comparisons of their tissues with those of Cycas revoluta.
It is probable, however, that when better known they will be found to
have a wider range of structure and affinities than we now suppose.

There are some reasons for believing that the trees described by
Corda under the names of Diplowylon, Myelopithys, and Heterangium,
and also the Anabathra of Witham, are Sigillarie. Much of the
tissue discribed by Goeppert as Araucarites carbonarius is probably
also Sigillarian.

4, Calamodendron.—The plants of this genus are quite distinct
from Calamutes proper. A Calamodendron as usually seen is a striated
east with frequent cross lines or joints; but when the whole stem is
preserved, it is seen that this cast represents merely an internal pith-
cylinder, surrounded: by a woody cylinder composed in part of scalari-
form or reticulated vessels, and in part of wood-cells with one row
of large pores-on each side.. External to the wood was a cellular bark,
and the outer surface seems‘to have been simply ribbed in the manner
of Sigdlaria. It so happens that the internal cast of the pith of —
Calamodendron, which is really.of the nature of a Sternbergia, so
closely resembles the external appearance of the true Calamites as to
be constantly mistaken for them. Most of these pith-cylinders of
Calamodendron have been grouped in the species Calamites approx-
matus; but that species, as understood by some authors, appears also
to include true Calamites*, which, however, when well preserved, can
always be distinguished by the scars of the leaves or branchlets which
were attached to the nodes.

Calamodendron would seem, from its structure, to have been closely
allied to Srgillaria, though, according to Unger, the tissues were dif-

* See Geinitz, ‘‘ Steinkohlenformation in Sachsen.”

1865.] | DAWSON—COAL-FORMATION. | 135

ferently arranged, and the woody Ses must have been much
thicker in proportion.

The tissues of Calamodendron are by no means infrequent in the
coal, and casts of the pith are common in the sandstones; but its
foliage and fruit are unknown. (Fig. 31, Pl. VII., a to eh

5. Calamites.—Nine species of true Calamites have been recognized
in Nova Scotia, of which seven occur at the Joggins, the most abundant
being C. Suckovii and C. Cisttz. ‘The Calamites grew in dense brakes
on sandy and muddy flats. ‘They were unquestionably allied to Hqui-
setacece, and produced at their nodes either verticillate simple linear
leaves, as in C. Crist, or verticillate branchlets with pinnate or verticil-
late leaflets, as in C. Suckovii and C. nodosus. The Calamites do not
seem to have contributed much to the growth of coal, though their
remains are not infrequent in it. The soils in which they most fre-
quently grew were apparently too wet and liable to inundation and
silting up to be favourable to coal-accumulation. I have elsewhere
shown that some of the species of Calamites gave off numerous ad-
ventitious roots from the lower parts of their stems, and also multi-
plied by budding at their bases*.

Of the genus Hquisetites one species has been found in Cape Breton;
but it lias not as yet been recognized at the Joggins. (Fig. 88, Pl.
XIT.)

6. Asterophyllites, &c.
nularia, five of Sphenophyllum, and three of Pinnularia, have been
found in Nova Scotia. I place these together as probably allied
plants. The Pinnularie were apparently slender roots, with thin
epidermis, cellular bark, and a central axis. The others were pro-
bably low plants growing in wet places. I am not aware that
they contributed to any great extent to the accumulation of coal; but
as their tissues were scalariform, similar to those of ferns, it would
not be easy to recognize them. A beautiful specimen of Spheno-
phyllum emarginatum from New Brunswick, in the collection of Sir
W.E. Logan, has enabled me to ascertain that its stem had a simple
axis.of one bundle of reticulato-scalariform vessels, like those of Z’me-
sypteris as figured by Brongniart. These curious plants were no
doubt cryptogamous, having a habit of growth like that of Hquise-
tacee, leaves like those of ferns or Marsilacce, and fructification
and structure like those of Lycopodiacew. They were closely allied
to Asterophyllites and Annularia.

7. Filices—Of the numerous species of ferns in the Carboniferous
rocks of Nova Scotia, only a very few have been recognized at the Jog-
gins. This may in part be due to the soft and crumbling character
of the shales; but after much examination I am inclined to believe that
the flora of the Joggins was originally poor in ferns. While the
coal-field of Sydney, Cape Breton, has afforded forty-six species,
the Joggins and its vicinity have as yet yielded only six or seven.
Of these by far the most abundant is Alethopteris lonchitica, which ap-_
pears throughout the Middle Coal-formation under a oreat number
of varietal forms. It is also found abundantly at Springhill. At

* Quart. Journ. Geol. Soc. vol. x. p. 34

L2

136 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Deen20;

Sydney, on the contrary, Pecopteris abbreviata and Alethopteris ner-
vosa are the most common ferns. But though fronds of ferns are
comparatively rare at the Joggins, except in a few beds, and these
holding principally the species Alethopteris lonchitica, bundles of
scalariform vessels referable to ferns occur very plentifully in the
coarser parts of the coal-beds, and would seem to indicate that vast
quantities of stipes and fronds have been resolved into coal. It is
to be observed, however, that it is not in all cases possible to di-
stinguish the vascular bundles of ferns from those of the leaves of
Sigillarioid and Lycopodiaceous plants. (Fig. 67, Pl. XII.)

Trunks of two species of tree ferns of the genus Palwopteris have
been found in Nova Scotia and New Brunswick, and also. obscure
fragments, probably of Cawlopteris and Psaronius. (Figs. 35 & 36,
Pl. VIII.)

8. Megaphyton.—These are perhaps the most curious and puzzling

plants of the coal. Their thick stems, marked by linear scars and
having two rows of large depressed areoles on the sides, suggest no
affinities to any known plants. They are usually ranked with Lepi-
dodendron and Ulodendron, but sometimes, and probably with
greater reason, are regarded as allied to tree ferns. At the Joggins
a very fine species (1. magnificum) has been found, and at Sydney a
smaller species (IZ. humile) ; but both are rare and not well preserved.
If the large scars supported cones and the smaller leaves, then, as
Brongniart remarks, the plant would much resemble Lepidophlovos, in
which the cone-scars are thus sometimes distichous. But the scars
are not round and marked with radiating scales as in Lepidophlovos ;
they are reniform or oval, and resemble those of tree ferns, for
which reason they may be regarded as more probably leaf-scars* ;
and in that case the smaller linear scars would indicate ramenta, or
small aérial roots. Further, the plant described by Corda as Zippea
disticha is evidently a Megaphyton, and the structure of that species
is plainly that of a tree fern of somewhat peculiar type. On these
grounds I incline to the opinion of Geinitz, that these curious trees
were allied to ferns, and bore two rows of large fronds, the trunks
being covered with coarse hairs or small aérial roots. At one time
I was disposed to suspect that they may have crept along the ground ;
but a specimen from Sydney shows the leaf-stalks proceeding from
the stem at an angle so acute that the stem must, I think, have been
erect. From the appearance of the scars it is probable that only a
pair of fronds were borne at one time at the top of the stem; and if
these were broad and spreading, it would be a very graceful plant.
To what extent plants of this type contributed to the accumulation
of coal I have no means of ascertaining, their tissues in the state
of coal not being distinguishable from those of ferns and Lyco-
podiacec. ;
_ The species Megaphyton humile had, like Corda’s Zippea disticha,
a thick central axis striated longitudinally, and giving off very thick
bundles of fibres, and probably scalariform vessels, to the bases of
the leaves. (Figs. 33 & 34, Pl. VIII.)

* This is the view of Lindley, ‘ Fossil Flora,’ p. 116.

1865. | _ DAWSON—COAL-FORMATION, 137

9. Lepidodendron.—Of this genus nineteen species have been re-
corded as occurring in the Carboniferous rocks of Nova Scotia. Of
these, six occur at the Joggins, where specimens of this genus are very
much less abundant than those of Sigillarta. In the newer Coal-
formation Lepidodendra are particularly rare, and L. wndulatum is
the most common species. In the Middle Coal- formation L. rimo-
sum, L. dichotomum, L. elegans, and L. Pictoense are probably the
most common species; and L. corrugatum is the characteristic Lepi-
dodendron of the Lower Carboniferous, in which plants of this species
seem to be more abundant than any other vegetable remains whatever.

To the natural history of this well-known genus I have little to
add, except in relation to the changes which take place in its trunk
in the process of growth, and the study of which is important in
order to prevent the undue multiplication of species. These are of
three kinds. In some species the areoles, at first close together,
become, in the process of the expansion of the stem, separated by in-
teryening spaces of bark in a perfectly regular manner; so that in
old stems, while widely separated, they still retain their arrange-
ment, while in young stems they are quite close to one another.
This is the case in L. corrugatum (Pl. XI.). In other species the
leaf-scars or areoles increase in size in the old stems, still retaining
their forms and their contiguity to each other. This is the case in
L. undulatum, and generally in those Lepidodendra which have very
large areoles. In these species the continued vitality of the bark is
sbown by the occasional production of lateral strobiles on large
branches, in the manner of the modern Red Pine of America. In
other species the areoles neither increase in size nor become regularly
separated by growth of the intervening bark; but in old stems the
bark splits into deep furrows, between which may be seen portions
of bark still retaining the areoles in their original dimensions and
arrangement. This is the case with LZ. Pictoense. This cracking of
the bark no doubt occurs in very old trunks of the first two types,
but not at all to the same extent. I figure three examples of these
peculiarities in mode of growth :—

Lepidodendron corrugatum, Dawson.—I quote in the Appendix
my description of this species, and may refer to the figures in Plate
XI. for further illustration. I do not know any other species in
Nova Scotia which has the same habit of growth; but Z. oculatum
and L. distans of Lesquereux show a tendency to it. The present
species is exclusively Lower Carboniferous, and occurs on that
horizon in New Brunswick, in Pennsylvania, and, I believe, also in
Ohio; though the beds holding it in the latter State have been by
some ‘regarded as Devonian.

L. Wiachuletuine: Sternberg.—I think it not improbable that several
closely allied species are included under this name. On the other
hand, all the large-areoled Lepidodendra figured in the books must
have branches with small scars, which, in the present: state of know-
ledge, it is impossible to identify with this species. I suppose that Z.
elegans resembles the present species in its mode of growth, at least
if the large-scarred specimens attributed toit are really of the same

188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Dec. 20,

species. L. dichotomum (=L. Sternbergic) also resembles it to some
extent. (Hig. 41, Pl. IX.) -

L. Pictoense, Dawson.—This species I described as follows, from
young stems, in my “Synopsis of the Coal-Plants of Nova Scotia:”—
“Areoles contiguous, prominent, separated in young stems by a
narrow line, long-oval, acuminate; breadth to length as 1 to 3 or
less; lower half obliquely wrinkled, especially at one side. Middle
line indistinct. Leaf-scar at upper end of areole, small, triangular,
with traces of three vascular points, nearly confluent. Length of
areole about 0-5 inch.” |

Additional specimens from Sydney show that in old trunks of this

species the areoles do not enlarge, but the bark becomes split into
strips. JI have reason to think that a new species from Nova Scotia
which I have described in the Appendix, L. personatwm, agrees with
it in this respect. (Figs. 37, 38, and 39, Pl. IX.)
_ The Lepidodendra resemble each other too closely to admit of good
subgeneric distinction. The grounds on which the distinction of
Sagenaria and Aspidiaria is founded are quite worthless, the ap-
parent position of the vascular scars in the areoles depending on
accidents of preservation much more than on original differences.
The genus Anorria includes many peculiar conditions of decorticated
Lepidodendru.

In regard to the accumulation of coal, Lepidodendra, when pre-
sent, appear under the same conditions with Sigillarie, the outer
bark being converted into shining coal, and the scalariform axis
appearing as mineral charcoal of a more loose and powdery quality
than that derived from Sigillaria. On the planes of lamination of
the coal the furrowed bark of old trunks can scarcely be dis-
tinguished from that of old Stgillaric.

10. Lepidophlovos.—Under this generic name, established by Stern-
berg, I propose to include those Lycopodiaceous trees of the Coal-
measures which have thick branches, transversely elongated leaf-
sears, each with three vascular poits and placed on elevated or
scale-hke protuberances, long one-nerved leaves, and large lateral
strobiles in vertical rows or spirally disposed. Their structure
resembles that of Lepidodendron, consisting of a Sternbergia pith, a
slender axis of large scalariform vessels, giving off from its surface
bundles of smaller vessels to the leaves, a very thick cellular bark,
anda thin dense outer bark, having some elongated cells or bast
tissue on its inner side.

Regarding L. laricinwm of Sternberg as the type of the genus, and
taking in connexion with this the species described by Goldenberg,
and my own observations on numerous specimens found in Nova
Scotia, I have no doubt that Lomatophloios crassicaulis of Corda, and
other species of that genus described by Goldenberg, Ulodendron
and Bothrodendron of Lindley, Lepidodendron ornatissimum of Brong-
niart, and Halonia punctata of Geinitz all belong to this genus, and
differ from each other only in conditions ef growth and preservation.
Several of the species of Lepidostrobus and Lepidophyllum ‘also
belong to Lepidophioios. Selages

1865. ] % DAWSON—COAL-FORMATION, 139

_ The species of Lepzdophlovs are readily distinguished from Lepi-
dodendron by the form of the areoles, and by the round scars on the
stem, which usually mark the insertion of the strobiles, though in
barren stems they may also have produced branches; still the fact of
my finding the strobiles 7m stu in one instance, the accurate resem-
blance which the scars bear to those left by the cones of the Red Pine
when borne on thick branches, and the actual impressions of the
radiating scales in some specimens, leave no doubt in my mind that
they are usually the marks of cones; andthe great size of the cones
of Lepidophloios accords with this conclusion.

The species of Lepidophloios are numerous, and individuals are

quite abundant in the Coal-formation, especially toward its upper
part. Their flattened bark is frequent in the coal-beds and their
roofs, affording a thin layer of pure coal, which sometimes shows the
peculiar laminated or scaly character of the bark when other charac-
ters are almost entirely obliterated. The leaves also are nearly as
abuudant as those of Sigillaria in the coal-shales, They can readily
be distinguished by their strong angular midrib.
_ I figure, in illustration of the genus, all the parts known to me of*
LL, Acadianus, and characteristic specimens of other species. One of
these, L. parvus, is characteristic of the Upper Coal-formation. (Vide
Flaite X. & Plate XI. fig. 51.)

11. Cordaites or Pychnophyllum.—this plant is represented in the
Coal-formation chiefly by its broad striated leaves, which are
extremely abundant in the coal and its associated shales. Some
thin coals are indeed almost entirely composed of them. The most
common species is C. borassifolia, a plant which Corda has shown to
have a simple stem with a slender axis of scalariform vessels resem-
bling that of Lepidophloios; for this reason, notwithstanding the
broad and parallel-veined leaves, I regard this genus as belonging
to Lycopodiacece or some allied family. It must have been extremely
abundant in the Carboniferous swamps ; and, from the frequency of
its being covered with Spirorbis, I think it must either have been of
more aquatic habit than most of the other plants of the Coal-forma-
tion, or that its leaves must have been very durable. While the
leaves are abundant, the stems are very rare. I infer that they were
usually low and succulent. Much of the tissue found in the coal,
which I have called “epidermal,” probably belongs to leaves of
Cordartes.

In the Upper Coal-formation there is a second species, distinguished
by its simple and uniform venation. This I have named C. sim-
plex.

12. Sporangites.—To avoid the confusion which envelopes the clas-
sification of Carpolites, I have used the above name for rounded spore-
cases of Lepidodendron and allied plants, which are very frequent
in the coal. A smooth round species like a mustard-seed, is exces-
sively abundant in the Lower Carboniferous at Horton, and probably
belongs to Lepidodendron corrugatum, with which it is associated.
A species covered with papille, S. papillata, constitutes nearly the
whole of some layers in coal 12, group xix, of the preceding Section.

140 PROCEEDINGS OF THE GLOLOGICAL SOCIETY. [Dec. 20,

I have no indication as to the plant to which it may belong, except
that it is associated with Cordaites. (Figs. 80 & 81, Pl. XITI.)*

13. Tissues in the Mineral Charcoal.—On these I have little to add
to the statements in my paper of 1859, “‘ On the Vegetable Structures
in Coal”;. These tissues may be arranged as follows :—

a. Bast tissue, or elongated cells from the liber or inner bark of
Sigillariz and Lepidodendron, but especially of the former.—This
kind of tissue is abundant in a calcified state in the shales associated
with the coals, and also as mineral charcoal in the coals themselves,
and in the interior of erect Sigillarie. It is the kind of tissue
figured by Brongniart as the inner layer of bark in Sigillaria
elegans, and very well described by Binney (Quart. Journ. Geol. Soc.
vol. xviii.) as “ elongated tissue or utricles.”’ Under the microscope
many specimens of it closely resemble the imperfect bast tissue of
the inner bark of Pinus strobus and Tha occidentalis ; and like this
it seems to have been at once tough and durable, remaining in
fibrous strips after the woody tissues had decayed. It is extremely
abundant at the Joggins in the mineral charcoal of the smaller
coal-seams. It is often associated with films of structureless coal,
which represent the dense cellular outer bark which, in the trunk
of Sigellaria, not only surrounded this tissue, but was intermixed with
it.) (Hig. 62, Pi ls)

b. Vascular bundles of Ferns. _These x may be noticed by all close
observers of the surfaces of coal, as slender hair-like fibres, some- __
times:lying separately, in other cases grouped in bands half an inch or
more in diameter, and imbedded in a loose sort of mineral charcoal.
When treated with nitric acid, each bundle resolves itself into a few
scalariform vessels surrounded with a sheath of woody fibres, often
minutely porous. This structure is precisely that of macerated fern-
stipes ; but, as already stated, there may have been some other coal-
plants whose leaves presented similar bundles. As stated in my for-
mer paper “ On the Vegetable Structures in Coal,” this kind of tissue
is especially abundant in the coarse and laminated portions of the
coal, which we know on other evidence to have been made up, not
of trunks of trees, puby ot mixed herbaceous matters. (Pl. XII.
fig. 67. yi

ce. Scalar ifor m vessels.—These are very abundant in the mineral
charcoal, though the coarser kinds have been crushed and broken in
such a manner that they usually appear as mere débris. . The sca-
lariform vessels of Lepidodendron, Lepidophlotios, and Stigmaria are
very coarse and much resemble each other. Those of ferns are
finer, and sometimes haye a reticulated structure. Those of Sigil-
daria are much finer and often have the aspect of wood-cells with
transversely elongated pores like those of Cycas. Good examples of
these are floured i in the paper already referred to. (See also Plate
XI. figs. 54, &¢.)
d. Discigerous wood-cells——These are the true bordered porcs
* Tt much rescmbles the spore-cases of Flemingites gracilis, as figured by Car-

ruthers, ‘Geol. Mag.’ vol. 1. I suppose this to be a strobile of Lepidophloios.
Tt Quart, Journ. Geol. Soc. February 1860.

1865. | ; DAWSON—COAL-FORMATION, 141

characteristic of Sigillaria, Calamodendron, and Dadoxylon. In the
two former genera the disks or pores are large and irregularly ar-
ranged, either in one row or several rows. In the latter case they
are sometimes regularly alternate and contiguous. In the genus
Dadoxylon they are of smaller size and always regularly contiguous
in two or more rows, so as to present an hexagonal areolation. Dis-
cigerous structures of Sigillaria and Calamodendron are very abun-
dant in the coal, and numerous examples were figured in my former
paper. I have indicated by the name fLeticulated Tissue certain
cells or vessels which may either be reticulated scalariform vessels,
or an imperfect form of discigerous tissue. I believe them to belong
to Stigmaria or Calamodendron. (Figs. 57 & 68, Pl. XIT.)

e. Epidermal tissue.—This is a dense cellular tissue representing
the outer integuments of various leaves, herbaceous stems, and fruits.
I have ascertained that the structures in question occur in the leaves
and stipes of Cordaites and ferns, andin the outer coat of Carpolites
and Sporangites. With this I may include the obscure and thick-
walled cellular tissue of the outer bark of Sigillaria and Lepidoden-
dron and other trees, which, though usually consolidated into com-
pact coal, sometimes exhibits its structure.

I would here emphatically state that all my observations at the
Joggins confirm the conclusion, which I arrived at many years ago
from the study of the coals of Pictou and Sydney, that the layers
of clear shining coal (pitch or cherry coal) are composed of flattened
trunks of trees, and that of these usually the bark alone remains ;
further that the lamination of the coal is due to the superposition of
layers of such flattened trunks alternating with the accumulations of
vegetable matter of successive years, and occasionally with fine vege-
table muck or mud spread over the surface by rains or by inundations.
In connexion with this, it is to be observed that the density and im-
permeabihty of cortical tissues not only enable them to endure after
wood has perished or been resolved into bits of charcoal, but render
them less liable than the wood to mineral znjiltration.

14. Rate of Growth of Carboniferous Plants.—Very vague statc-
ments are often made as to the supposed rapid rate of growth of plants
in the Carboniferous period. Perhaps the most trustworthy facts in
relation to this subject are those which may be obtained from the
coniferous trees. In some of these (for instance, Dadoxylon materi-
arium, D. annulatum, and D. antiquius) the rings of growth, which
were no doubt annual, are distinctly marked. On measuring these
in a number of specimens, and comparing them with mcdern species,
I find that they are about equal in dimensions to those of the
Balsam-Fir or the Yellow Pine of America. Assuming, there-
fore, similarity in habit of growth and extent of foliage to these
species, we may infer that, in regard to coniferous trees, the
ordinary conditions of growth were not dissimilar from those of
Eastern America in its temperate regions at present. When, how-

ever, we compare the ferns and Lycopodiacee of the Coal-formation
with those now growing in Eastern America, we see, in the much
greater dimensions and luxuriance of the former, evidence of a much

142 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

more moist and equable climate than that which now subsists;
so that we may suppose the growth of such plants to have been
more rapid than it is at present. These plants would thus lead us
to infer a warm and insular climate, perhaps influenced by that sup-
posed excess of carbonic acid in the atmosphere, which, as Tyndall
and Hunt inform us, would promote warmth and moisture by im-
peding terrestrial radiation. With this would also agree the fact
that the Conifers have woody tissues resembling those of the pine
trees of the milder climates of the southern hemisphere at present.

If we apply these considerations to Sigidlaria, we may infer that
the conditions of moisture and uniformity of temperature favourable
to ferns and Lycopodiacew were also favourable to these curious
plants. They must have been perennial ; and the resemblance of their
trunks to those of Cycads, together with their hard and narrow
leaves, would lead us to infer that their growth must have been very
slow. A similar inference may be drawn from the evidences of very
slow and regular expansion presented by the lower parts of their
stems. On the other hand, the distance, of a foot or more, which
often intervenes between the transverse rows of scars, marking pro-
bably annual fructification, would indicate a more rapid rate of
growth. Further, it may be inferred, from the structure of their
roots and of their thick inner bark, that these, as in Cycads, were re-
ceptacles for great quantities of starch, and that the lives of these
plants presented alternations of starch-accumulation and of expen-
diture of this in the production of leaves, wood, and abundant inflo-
rescence. ‘They would thus, perhaps for several years, grow very
slowly, and then put forth a great mass of fructification, after which
perhaps many of the individuals would die, or again remain for a long
time in an inactive state. This view would, I think, very well har-
monize with the structure of these plants, and also with the mode of
their entombment in the coal.

From the manner of the association of Calamites with erect Sagil-
lari, I infer that the former were, of all the plants of the Coal-for-
mation, those of most rapid dissemination and growth. They appear
to have first taken possession of emerging banks of sand and mud,
to have promoted the accumulation of sediment on imundated
areas, and to have protected the exposed margins of the forests of
Sigillarice.

In applying any conclusions as to the rate of growth of Carboni-
ferous plants to the accumulation of coal, we must take into account
the probable rate of decay of vegetable matter. When we consider
the probable wetness of the soils on which the plants which pro-
duced the coal grew, the density of the forests, and the possible
excess of carbonic acid in the atmosphere of these swamps, we must
be prepared to admit that, notwithstanding the warmth and humidity,
the conditions must have been favourable to the preservation of ve-
getable matter.. Still the hollow cylinders of bark, the little frag-
ments of decayed wood in the form of mineral charcoal, and the
detached vascular bundles of ferns, testify to an enormous amount of
decay, and show that, however great the accumulation of coal, it

1865.) _ é DAWSON—COAL-FORMATION, 143

represents only a fraction of the vegetable matter which was actually
produced. It has been estimated that it would require eight feet of
compact vegetable matter to produce one foot of coal*; but if we
reckon the whole vegetable matter actually produced in the process,
I should suppose that five times that amount would be far below
the truth, even in the most favourable cases ; while there is evidence
that in the Carboniferous period many forests may have flourished for
centuries without producing an inch of coaly matter.

15. Bivalve Shells —A1l the Lamellibranchiate shells, which are
so numerous in some of the shales and bituminous limestones of the
Joggins that some of the beds may be regarded as composed of
them, belong to one generic or family group. They are the so-
called Modiolas, Unios, or Anodons of authors. I proposed for them
some years ago the generic name of Naradites, and described six
species from the Coal-measures of Nova Scotia, stating my belief
that they are allied to Uniomde, and that their nearest analogue may
be the genus Bysso-anodonta of D’Orbigny, found in the River Pa-
panay. Mr. Salter, however, to whom I sent specimens, regards
these shells as belonging to his new genera Anthracomya and Anthra-
coptera, the former being supposed to be allied to Myadet. More
recently Giimbel and Geinitz have described similar shells from
Thuringia as belonging to the genera Unio and Anodon, and regard
my Naadites carbonarius (Anthracoptera carbonaria of Salter) as a
Dreissena§. As these shells swarmed in the waters of the Coal-for-
mation estuaries or lagoons, facts tending to the elucidation of their
habits and affinities are important with reference to the coal; I would
therefore make the following remarks in relation to them :—

(1) Under the microscope, the shells of the thicker species, as Naia-
dites carbonarius, present an internal lamellar and subnacreous layer,
a thin layer of vertical prismatic shell, and an epidermis—these
structures being entirely similar to those of Unionide. In the
thinner species, as in WV. levis, only the prismatic coat appears, and
in this the prisms are in some instances placed obliquely. These
thin shells, however, show evidence of an epidermis. (2) The
ligament was external, there seem to have been no teeth, the shell
was closed posteriorly ; but there are indications of a byssal sinus.
Mr. Salter describes the epidermis as wrinkled posteriorly ; but this,
with the exception of the rings of growth, appears to me to result
from pressure. The shells are equivalve, and have the external
aspect of Unionde or Mytilide. (3) I know of no instance in
Nova Scotia of the occurrence of these shells in the strictly marine
limestones, nor have any properly marine forms of Mollusca been
found with Naiadites.in the Coal-measures. (4) The mode of their
oceurrence precludes the idea that they were burrowers, but favours
the belief that they were attached by a byssus to sunken or floating
timber. On the whole I think that the balance of probability is in

* Dana’s Manual, p. 367.

t Supplement to Acadian Geology, 1860.

{ Quart. Journ. Geol. Soe. vol. xix. p. 79.

§ Neues Jahrbach, 1864. Geological Magazine, May 1865.

144 PROCERDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

favour of the conclusion that they were brackish-water or fresh-
water shells, allied to Mytilde or to embryonic Unionide.

16. Spirorbis carbonarius.—This little shell, which I described as
a Spirorbis as long ago as 1845*, is apparently not specifically distinct
from Microconchus carbonarius of the British coal-fields. Its micro-
scopic structure is identical with that of modern Spirorbes, and shows
that it is a true worm-shell. It is found throughout the Coal-
formation, attached to plants and to shells of Navadites, and must
have been an inhabitant of enclosed lagoons and estuaries. Its
occurrence on Sigillarie has been used as an argument in favour of
the opinion that these trees grew in sea-water; but, unfortunately
for that conclusion, the Spzrorbis is often found on the inside of Sigz-
laria-bark, showing that this had become dead and hollow. Beside
this, the same kind of evidence would prove that Lepidodendra, Cor-
daites, and Ferns were marine plants. Spirorbes multiply fast and
grow very rapidly; and these little shells no doubt took immediate
possession of submerged vegetation, just as their modern allies cover
fronds of Laminaria and Fucus. :

As I have not met with a description of this little shell, I may
state that it is dextral, with 24 to 3turns. It is attached through-
out its length, and when not compressed presents a somewhat deep
umbilicus. It is closely marked with beaded or unequal transverse
ridges. It has when young a close resemblance to Sp. caperatus,
M‘Coy, from the Carboniferous Limestone of Ireland ; but this species
has only two turns, and is sinistral.

17. Orustacea.—lt appears in the table above that as many as four-
teen beds of coal exhibit in their roofs shells of minute Entomostraca
of the genera Cythere and Bairdia; and these occur in such quan-
tities that considerable beds of shale and bituminous limestone are
filled with their valves. Professor Jones regards the species as
marine or brackish-water; and the same remark will, I presume,
apply to the crustacean Diplostylus Dawson, and a fragment of
Eurypterus described by Mr. Salter from Coal no. 8 of Division 4
of the Section. Of the small Entomostracans there are several
species, which Professor Jones has now in his hands for determina-
tion. No Estherians have yet been found in the Coal-formation of
Nova Scotia; but I have specimens of Leaia Leidyi from the Lower
Carboniferous of Plaister Cove, and an undetermined Hstheria from
the same horizon at Horton Bluff. .

It is to be observed that Nacadites, Spirorbis, and Cythere con-
stantly occur associated in the same beds ; and the conclusions as to
habitat applicable to any one of these genera must apply to all.

18. Fishes—Remains of fishes occur in connexion with eighteen
of the coal-beds at the Joggins, usually in the roof-shales, though
detached scales, teeth, spines, or coprolites are of occasional though
rare occurrence in the coal itself, especially where the latter passes
into coarse’ coal or carbonaceous shale. One thin bed, no. 6 of
Division 4 of the Section, is full of remains of small fishes. It is
hard and laminated, and roofed with a calcareous bed full of remains

* Quart. Journ. Geol. Soc. vol. i. p. 326.

6

1865. | DAWSON—COAL-FORMATION. 145

of aquatic animals. It has a true Stigmarian underclay. I suppose
it to have been a swamp or forest submerged and occupied by fishes
while its vegetation was still standing. It contains remains of fishes
of the genera Ctenoptychius, Diplodus, Rhizodus, and Palewonscus.
It also contains Oythere, Naiadites, and Spirorbis. In the other -
beds which contain fish-remains, most of these consist of small Lepi-
doganoids, but there are occasional teeth and scales of large species
of Rhizodus, and also teeth and scales of Selachian fishes of consider-
able size.

19. Land-animals.—The Coal-formation of Nova Scotia has afforded
the remains of eight species of Reptiles or Batrachians, belonging to
the genera Hylonomus, Baphetes, Dendrerpeton, Hylerpeton, and Eosau-
gus ; of one Myriapod, Xylobius sigillarie; of one land snail, Pupa
vetusta ; and of one insect. All of these, except one of the reptiles,
have been found at the Joggins. I have nothing in regard to them
to add to what I have already published in my Memoir on ‘ Air-
breathers of the Coal Period.’

VY. APPENDIX.
Descriptive List of Carboniferous Plants found in Nova Scotia and
New Brunswick.

[Abridged and corrected from “ Synopsis of the Carboniferous Flora of Nova
Scotia,’ Can. Nat. vol. viii.] *

Dapoxyton, Unger.

1. Dapoxyron Acapranum, spec. nov. PI. V. figs. 4-6.

Large trees, usually silicified or calcified, with very wide wood-
cells, having three or more rows of small hexagonal areoles, cach
enclosing an oval pore; cells of medullary rays one-third of br@dth
of wood-cells, and consisting of twenty or more rows of cells super-
imposed in two series. Rings of growth indistinct.

M. C.t, Joggins, Port Hood, Dorchester (J. W. D.).

2. D. MATERIARIUM, spec. nov. (PLY. figs. 7-9.

Wood-cells less wide than those of the last; two to rarely four
rows of hexagonal disks.. Medullary rays very numerous, with
twenty or more rows of cells superimposed in one series. Rings of
growth slightly marked. Approaches in the character of its woody
fibre to D. Brandlingii; but the medullary rays are much longer.
Some specimens show a large Sternbergian pith, with transverse
partitionst. Vast numbers of trunks of this species occur in some
sandstones of the Upper Coal-formation.

M. and U. C., Joggins, Malagash, Pictou, &c. (J. W.D.); Glace
Bay (4. Poole) ; Miramichi (G. PF. Aatthew).

* The illustrations are principally from photographs by my son George M.
Dawson, and for the sake of economy have been confined to small and character-
istic portions of the specimens. .

t U.C., M.C., and L. C., indicate the Upper, Middle, and Lower Coal-for-

mations.
¢ Canadian Naturalist, 1857,

146 PROCEEDINGS OF THE GEOLOGICAL society. [ Dec. 20,

3. D. antrauius, spec. nov. PI. V. figs. 1-3.

Wood-cells narrow, thick-walled, two to three rows of pores. —
Medullary rays of three or four series of cells with twenty or more
superimposed, nearly as wide as the wood-cells. Rings of growth
visible. This species would belong to the genus Paleoxylon of
Brongniart, and is closely allied to D. Withami, L. and H., which,
like it, occurs in the Lower Coal-measures.

L. C., Horton (Dr. Harding).

4, D. annuzatum, spec. nov. Pl. V. figs. 10-18.

Wood-cells with two or three rows of hexagonal disks. Medul-
lary rays of twenty or more rows of cells superimposed, in two
series. Wood divided into distinct concentric circles, alternating
with layers of structureless coal representing cellular tissue or very
dense wood. <A stem 6 inches in diameter has fourteen to sixteen
of these rings, and a pyritized pith about Linchin diameter. ‘This is
probably generically distinct from the preceding species.

M. C., Joggins (Sir W. H. Logan; J. W. D.).

ARavcaritses, Unger.

ARAUCARITES GRACIZIS, ‘spec. noy. Pl. VI. fig. 14.

Branches slender, 0-2 inch in diameter, with scaly, broad leaf-
bases. Branchlets pinnate, numerous, very slender, with small,
acute, spirally disposed leaves.

U. C., Tatamagouche (J. W. D.).

SIGILLARTA, Brongn.
1. Sremuarra (Favurarta) exee¢ans, Brongn. Pl. VII. fig. 26.
Abundant, especially in the roofs of coal-seams. S. heaagona
includes old trunks of this species. Young branches have scars of
an elliptical form like those of S. Serli.
M. C., Joggins (J. W. D.); Sydney (2. Brown).
2. 8. (Fav.) vesserzara, Brongn.
M. C., Joggins and Pictou (J. W. D.); Sydney (2. Brown).
83. 8. (Ruyrrporzpis) scvrernaTa, Brongn. PI. VI. fig. 25.
M. and U. C., Joggins (Lyell; J. W. D.).
4, §. (Ru.) Scutoruemrana, Brongn.
M. C., Joggins (Lyell; J. W. D.).
5, §. (Ra.) Savzx, Brongn.
M. C., Sydney (2. Brown); Joggins (Lyell; J. W. D.).
6. 8. Browni1, Dawson (Quart. Journ. Geol. Soc. vol. x.). Pl. VI.
figs. 15-19.
M. C., Joggins (J. W. D.).
7. 8. genrFoRMIS, Brongn.
M. C., Joggins (Lyell; J. W.D.); Sydney (R. Brown).

1865. | DAWSON—COAL-FORMATION, 147

8. S. tavieaTa, Brongn.

M. C., Sydney (f. Brown); Joggins (J. W. D.).
9. S. PLANtcosra, spec. nov. Pl. VI. fig. 21.

Scars half hexagonal above, rounded below; lateral vascular im-
pressions elongate ; central small, punctiform. Ribs 1:1 inch broad,
smooth externally, longitudinally striated on the ligneous surface.
Slight transverse wrinkles between the scars, which are distant from
each other about an inch. Allied to S. levigata, but with very thin
bark.

M. C., Sydney (2. Brown).

10. S. catzenorpEs, spec. nov. Pl. VI. fig. 22.

Cortical surface unknown; ligneous surface with puncto-striate
ribs 1:1 inch in breadth, and with single oval scars half an inch long,
and an inch distant from centre to centre. A very large tree.
Perhaps, if its cortical surface were known, it might prove to be a
large Syringodendron.

M. C., Joggins (J. Snuth); Sydney (2. Brown).

11. 8. striata, spec. nov. Pl. VI. fig. 23.

Ribs prominent, coarsely striate, 0°35 inch wide. Scars nearly
as wide as the ribs, rounded, hexagonal, 1 inch distant; lateral vas-
cular marks narrow, central large. On the ligneous surface scars
single, round, oblong; bark very thin.

M. C., Joggins (J. W. D.).

12. 8. ?
A small erect stem, somewhat like S. flewuosa.
M. C., Joggins (J. W. D.).

13. 8, (CuatHRaria) Munarnt, Brongn.

M. C., Sydney (A. Brown); U. C., Pictou (J. W. D.).
14. 8.{(Asonanvs) Sypnensis, spec. nov. Pl. VII. fig. 28.

Ribs obsolete; cortical and ligneous surfaces striate; vascular
scars two, elongate longitudinally, and alike on cortical and ligneous
surfaces ; scars 1:1 inch distant, in rows 0-Ginch distant. Stigmarian
roots, same with variety h of Stigmaria, as described below.

M, C., Sydney (#. Brown).

15. S. orcanum, L. & H.
M. C., Sydney (#. Brown).
16. §. ntoneata, Brongn.
M. C., Sydney (R. Brown).
17. 8. rrmxvosa, L. & H.
_M.C., Sydney (2. Brown’s list in « Acadian Geology’).

18. S. pacnyprrma, L. & H.
M. C., Sydney (2. Brown’s list).

148 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

19. 8. (Fav.) Brerongnsts, spec. noy. Pl. VIL. fig. 27.

Like S. tessellata, but areoles more hexagonal, bark thin and smooth
on both sides, and furrow above the scars arcuate and with a central
punctiform elevation.

M. C., Sydney (R. Brown).

20. S: EMINENS, spec. nov. Pl. VI. fig. 24.

Like S. obovata, Lesqx., but with narrower ribs, and larger and
less distant areoles, each with a slight groove above.
M. C., Sydney (R. Brown).

21. S. Dovrnawsit, Brongn.
M. C., Joggins (J. W. D.).
22. S. Knorr, Brongn.
M. C., Sydney (2. Brown).

SYRINGODENDRON, Brongn.

Obscure specimens, referable to a narrow-ribbed species of this
genus, occur in the Lower Carboniferous beds at Horton and Onslow.

STIGMARIA, Brongn.
Srr¢MARIA FICOIDES, Brongn. Pl. XII. fig. 83-87.

Under this name I place all the roots of Sigillarie occurring in
the Carboniferous rocks of Nova Scotia. They belong, without
doubt, to the different species of Sigillarioid trees; but itis at present
impossible to determine to which ; and the specific characters of the
Stigmarie themselves are, as might be anticipated, evanescent and
unsatisfactory. The varieties which occur in Nova Scotia, discard-
ing mere difference of preservation, may be arranged as follows :—

Var. a. Areoles large, distant; bark more or less smooth. This is
the most common variety, and extends throughout the Coal-formation.

Var. b. Areoles large, separated by waving grooves of the bark.

Var.c. Similar, but ridges as well as furrows between the
areoles; var. undulata of Goeppert.

Var. d. Areoles small, separated by waving grooves.

Var. e. Areoles moderate, in vertical or diagonal furrows separated
by ridges ; var. sigillar ioides of Goeppert.

Var. if. “Areoles small ; bark finely netted with wrinkles or strie.

Var. g. Areoles surrounded by radiating marks, giving a star-
like form; var. stellata of Goeppert. The only specimen I have
seen was found by Dr. Harding in the Lower Carboniferous Coal-
. measures of Horton.

Var. h. Areoles small, or obscure and infrequent. Surface covered
with fine uneven strize. My specimens were collected by Mr. Brown
in the Middle Coal-measures at Sydney.

Var. 2. Areoles narrow, elongate, bark smooth or striate.

Var. k. alternans, with areoles in double rows on broad ribs sepa-
rated by deep furrows. Probably old furrowed roots.

1865. | DAWSON—COAL-FORMATION. 149

Var. 1, Knorroides. Prominent bosses or ridges instead of areoles.
These are imperfectly preserved specimens,

The varieties a, b, c, ¢,2, have been seen attached to trunks of
Sigillarice of the group distinguished by broad and prominent ribs—
Sigillaria proper of the above arrangement. Stigmaria, like Sigil-
laric, are exceedingly abundant in the Middle Coal-measures, and
are comparatively rare in the Lower Carboniferous and newer Coal-
formations.

CALAMODENDRON, Brongn.
1, CaLAMoDENDRON APPROxIMATUM, Brongn. PI. VII. fig. 31.

This plant is evidently quite distinct from Calamites proper. The
Calamite-like cast is a pith or internal cavity, surrounded by a thick
cylinder of woody tissue consisting of scalariform vessels and woody
fibres with one row of round pores; external to this is a bark of
cellular and bast tissue. The structure appears to be allied to that
of Sigillaria, and is one of the most common in the beds of bitu-
minous coal.

M. C., Sydney (R. Brown); M. C., Joggins, Pictou (J. W. D.);
Coal Creek (C. B. Matthew).

2. C. opscuruM, spec. nov. Pl. VII. fig. 31d.

This is a Calamite-like fragment found in a block of Sydney coal,
in the state of mineral charcoal. The external markings are obscure,
but the structure is well preserved. It differs from the last in
haying large ducts with many rows of pores, or reticulated instead
of sealariform vessels. This is perhaps a Calamite.

M. C., Sydney (J. W. D.).

Cyprritss, L. & H.

CYPERITES 2

These elongate linear leaves have two or three ribs, and the
central band between the ribs raised above the margin; one species
has been seen attached to Sigillaria Schlotheumiana.

The leaves of Stgillaria elegans are different, being as broad as
the areoles of the stem, and with several parallel veins.

Middle and upper coals, everywhere.

AntHotitHes, Brongn.

1. AntHoriraes Ruappocarrt, spec. nov. Pl. VII. fig. 30.

Stem short, interruptedly striate, with two rows of crowded ovate
fruits, and traces of floral leaves. Fruits half an inch long, striated
longitudinally, attached by short peduncles.

M. C., Grand Lake (C. F. Hartt).

2. A. premma, spec. nov. Pl. VII. fig. 30¢.

Rhachis 1 inch thick, rugose; two rows of opposite flowers, each
showing four lanceolate striate floral leaves, two outer and two
inner.

M.C., Joggins (J. W. D.).

VOL, XXII.—PART I. M

150 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

3. A. squamosa, spec. nov. Pl. VII. fig. 29.
Rhachis thick, coarsely rugose, with two rows of closely placed
cones or scaly fruits.
U. C., Pictou (J. W. D.).
4, A, ——?, spec. nov.
Indistinct, but apparently different from those above described.
M. C., Joggins (J. W. D.); Sydney (&. Brown).

TrigonocaRPum, Brongn.

1, TRiconocarpum Hooxerr, Dawson, Quart. Journ. Geol. Soc. vol.
XVil.
M. C., Mabou (J. W. D.).
2. T, SterLaRia, spec. nov. Pl. XII. fig. 76.

Ovate, 1 inch long; testa smooth, or rugose longitudinally, acu-
minate, two-edged. Found in erect trunks of Sigillarie in large
numbers.

M. C., Joggins (J. W. D.).

3. T. ivreRMEDIuM, spec. nov. Pl. XII. fig. 78.
Allied to T.“oliveformis, but larger and more elongated.
M. C., Joggins, (J. W. D.).

4, T. aveLtanum, spec, nov. Pl. XII[ffig. 77.

Allied to 7. ovatum, L. & H.; three-ribbed, size and form of a
filbert.

M. C., Joggins (J. W. D.); Sydney (#. Brown).
5. T. minus, spec. noy. Pl. XII. fig. 75.

Half the size of 7. Hookeri, and similar in form.

M. C., Joggins (J. W. D.).

6, T. RoTUNDUM, spec. Nov.
Small, round-ovate, slightly pointed.
M. C., Joggins (J. W. D.).
7. T. naceERaTHt, Brongn.
Newer Coal-formation, Pictou (J. W. D.).

Ruazpocarrus, Goepp. and Bergm.

1. Raaspocarpus —— ?, spec. nov.
Ovate acuminate, less than half an inch long.
M. C., Joggins (J. W. D.).

2. R. instenis, spec. nov. Pl. XII. fig. 69.

15 inch long, ovate, smooth, with about seven ribs on one side,
and the intervening surface obscurely striate. The nature of this
fossil is perhaps doubtful; but if a fruit, it is the largest I have
seen in the Coal-formation.

U. C., Pictou (J. W. D.).

1865. ] DAWSON-—COAL~FORMATION, 151

CazamiteEs, Suckow.

1. Catamrtes Sucxovir, Brongn.

This species is one of the most common in an erect position. It
has verticillate branchlets, with pinnate linear leaflets.

M.C., sae (R. Brown) ; Joggins (Lyell; J. W.D.); Grand Lake
(Coe Hartt); U .C., Pictou (J. W. D.); Coal Creek (C. B. Matthew).

2, C. Cistiz, Brongn.

M. C., Joggins (J. W. D.); Sydney (#. Brown); Grand Lake (C.F.
Hartt); Bay de Chaleur (Logan); Coal Creek (C. B. Matthew).

Often found erect. Its leaves are verticillate, simple, linear, striate,
apparently one-nerved, and 3 inches long.

3. C. cannz¥Formis, Brongn.
M. C., Joggins (Lyell; J. W. D.); Sydney (&. Brown).

4, C. ramosus, Artis.
Possibly a variety of C. Suckoviw.
M. C., Joggins (J. W. D.); Sydney (R. Brown).
5. C. Vorrziu, Brongn. (C. irregularis, L. & H.)
M.C., Joggins (J. W. D.). .
_ Often erect; has large irregular adventitious roots. This species
is regarded by Brongniart as probably belonging to Calamodendron.
6. C. pusrus, Artis.
M.C., Sydney (R. Brown); Joggins (J. W.D.; Logan); U.C., Pictou
(ol. 1...)
7. ©. Noya-scorica, spec. nov. Pl, XII. fig. 89.

M. C., Joggins (J. W. D.).

Ribs equal, less than a line wide, striated longitudinally. Joints
obscurely marked, and with circular areoles separated by the breadth
of three to four ribs. Bark of moderate thickness.

8. C. noposus, Schloth.

This species has long slender branchlets, with close whorls of

short rigid leaves.
M. C., Sydney (#. Brown); Grand Lake (C. F. Hartt).

9. C. ARENACEUS (?), Jiiger.
This species is mentioned with doubt in Lyell’s list.

Kauisetitss, Sternberg.

Eaurserrms cuRTA, spec. nov. Pl, XII. fig. 88.

Short thick stems, enlarging upward, and truncate above; joints
numerous; sheaths as long as the joints, with unequal acuminate
keeled points. Lateral branches or fruit with longer leaf-like
points. Has the characters of Hqwisetites ; but its affinities are quite
uncertain.

M.C., Sydney (R. Brown).

; M 2

152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

ASTEROPHYLLITES, Brongn.

1. AsTEROPHYLLITES FoLIosa, L. & H.

M. C., Joggins (J. W. D.); Sydney (£. Brown).
2. A. EquisEeTiForMIs, L. & H.

M. C., Sydney (2. Brown); Pictou (J. W. D.).
3. A. eRanpis, Sternberg ?

The specimens resemble this species, but are not certainly the
same. Logan’s specimens have terminal spikes of fructification.

M.C., Grand Lake (C. /. Hartt) ; Bay de Chaleur (Logan); Sydney
(Bunbury).
4, ASTEROPHYLLITES, sp.

A species with tubercles (fruit) in the axils is mentioned in
Lyell’s list as from Sydney. I have not seen it, but have a specimen
from Mr. Brown similar to A. tuberculata, Sternberg, which may be
the same.

5. A. TRINERVIS, spec. nov. Pl. XIII. fig. 90.

Main stem smooth, delicately striate, with leaves at the nodes.
Branches delicately striate, with numerous whorls of linear nearly
straight leaves, 0-5 inch long, twenty or more in a whorl, and show-
ing two lateral nerves in addition to the median nerve. This and
A, equisetiformis would be placed by some authors in Annularia.

M. C., Sydney (£. Brown).

ANNULARIA, Sternberg.
ANNULARIA GALIOIDES, Zenker.

M.C., Grand Lake (C.F. Hartt); U.C., Pictou(J. W. D.); Bay de
Chaleur (Logan); Sydney (2. Brown).

SPHENOPHYLLUM, Bronen.
1, SPHENOPHYLLUM EMARGINATUM, Brongn.
M. C., Sydney (2. Brown); Grand Lake (C. Ff. Hartt); Bay de
Chaleur (Logan) ; ; Pictou (/. W. D.).
2. S. Lonerrotium, Germar.
U.C., Pictou (J. W. D.); M.C., Sydney (2. Brown).
3. 8. SAXIFRAGIFOLIUM, Sternberg.

Elongate much-forked variety, closely allied to S. bifurcatum,
Lesquereux.

Bay de Chaleur (Logan).
4, §. ScunotHermir, Brongn.
M. C., Sydney (Bunbury).

5, 8. prosum, L. and H.

M. C., Sydney (Bunbury).
The last two species are regarded by Geinitz as varieties of S.
emargimatum., A specimen of the last-named species in Sir William

1865. | DAWSON—COAL-FORMATION. 153

| Logan’s collection shows a woody jointed stem like that of <Astero-
phyllites, giving off branches at the joints; these again branch and
bear whorls of leaves. The stem shows under the microscope a
single bundle of reticulated or scalariform vessels like those of some
ferns, and also like those of Z'mesipteris, as figured by Brongniart.
This settles the affinities of these plants as being with ferns or with
Lycopodiacee.
Prynvaria, L. & H.
1. PInNULARIA CAPILLACEA, L. & H.

M, C., Sydney (A. Brown).

2, P. RAMOSISSIMA, spec. nov.

More slender and ramose than the last.

M. C., Joggins (J. W. D.).
3. P. CRASSA, spec. Nov.

Branching like P. capillacea, but much stronger and coarser.

L. C., Horton (C. F. Hartt).

All these are apparently branching fibrous roots, of soft cellular
tissue with a thin epidermis and slender vascular axis. Perhaps
they are roots of Asterophyllites.

Genus Na@teerraTHiA, Sternberg.
1. Na@eeERATHIA DISPAR, spec. noy. Pl. XIII. fig. 91.

A remarkable fragment of a leaf, with a petiole nearly 3 inches
long, and a fourth of an inch wide, spreading abruptly into a lamina,
one side of which is much broader than the other, and with parallel
veins running up directly from the margin as from a marginal rib.
It appears to be doubled in at both edges, and is abruptly broken
off. It seems to be a new species; but of what affinities, it is im-
possible to decide.

Bay de Chaleur (Sir W. £. Logan).

2. N. ruapetiata, L. & H.
M. C., Sydney (2. Brown).

CycLopreris, Brongn.

(including Cyclopteris proper, and subgenera-Aneimites, Daws., and
Neuropteris, Brongn.).

1. CycLOPTERIS HETEROPHYLLA, Goeppert.

M. C. and U. C., Joggins (J. W. D.).

2. C. (AvzruirEs) Acapica, Dawson, Quart. Journ. Geol. Soc. vol.
xXyll. p. 0. Pl. VILL. fig. 32.

Stipe large, striate, branching dichotomously several times.
Pinnz with several broadly obovate pinnules grouped at the end of
a slender petiolule, and with dichotomous radiating veins. Fertile
pinne with recurved petiolules, and borne on the divisions of the
main petiole near their origin. This plant might be placed in the
genus Adiantites, Brongn., but for the fructification, which allies it

154 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Dec. 20,

with such ferns as Anemia. It has avery large frond, the main
petiole being sometimes 3 inches in diameter, and 2 feet long before
branching. Flattened petioles have sometimes been mistaken for
Cordaites and Schizopteris. It is a characteristic plant of the Lower

Coal-measures.
L. C., Horton (C.F. Hartt); Norton Creek, N.B.(G. F. Matthew).

3. C. optonerroria, Goeppert.
A little larger and coarser than Goeppert’s figure.
U. C., Pictou (J. W. D.).

4, C. (NEUROPTERIS) oBLIQUA, Brongn.
M.C., Sydney (2. Brown) ; Grand Lake (C. F. Hartt).

5. C. (?Nevropreris) neEns, L. & H.
. C., Sydney (A. Brown); Grand Lake (C. F. Harit).

. oBLATA, L. & H.
. C., Sydney (2. Brown).

C
M
7. C. rimpriata, Lesquereux.
M
C

Ss

. C., Sydney (2. Brown).

. HISPIDA, spec. nov. Pl. XIII. fig. 92.
Pinnate; pinnules obovate, diminishing in size towards the point,
decurrent on the petiole; veins slender, distant, forking several
times; under surface covered with stiff hairs.
M.C., Sydney (2. Brown),

9, C. anrrava, spec. nov. Pl. XIII. fig. 95.

L. C., ? Hebert River (J. W. D.).

Tripinnate ; petioles slender; pinnules oblong, obtuse, decurrent
on the petiole, not contiguous. Terminal pinnules much elongated ;
venation simple, divergent. This plant approaches more nearly to
the peculiar species of Cyclopterts found in the Devonian, than any
of the others I have seen in the Carboniferous,

8.

Nevropteris, Brongn.

1, NEUROPTERIS RARINERVIS, Bunbury.

M. C., Sydney (2. saniaitis Grand Lake (C. F. Hartt) ; Bay de Cha-
leur (Logan).

2. N. PERELEGANS, spec. nov. Pl. XIII, fig. 93.

M. C., Sydney (#. Brown).

Resembles NN. elegans, Brongn., but has narrower ‘pinnules, and
nerves less oblique to the midrib. The pinnules were thick and
leathery, rough or cellular-netted above, and showing the venation
only on the underside.

3. N. corpata, Brongn. (and var. angustifolia).

The ferns referred to this species are identical with WV. hirsuta
of Lesquereux. They abound in the Middle and Upper Coal-forma-
tions, and have larger pinnules than any of the other ferns, A

1865. ] DAWSON—COAL-FORMATION. 155

single terminal pinnule in my collection is 5 inches long. The sur-
face is always more or less hairy.

M. C., Sydney (#. Brown); U. C., Pictou (J. W. D.).
4, N. Vourzti, Brongn.

A single imperfect specimen like this species, but uncertain.
M. C., Pictou (J. W. D.).

5. N. ereantea, Sternb.

M. C., Sydney (2. Brown); Grand Lake (C. F. ue U.C., Pic-
tou (J. W. D.»).
6. N. ruexvosa, Sternb.

M. C., Sydney (2. Brown) ; Joggins (J. W. D.).

7. N. wereropnyiia, Brongn.
M. C., Sydney (R. Brown); U.C., Pictou (J. W. D.).
9. N. Losuiz, Brongn.
‘Bay de Chaleur (Logan).
10. N. acurrroria, Brongn.
M. C., Sydney (Lyell’s list).
11. N. consveata, Goepp.
M. C., Sydney (Brown’s list, Acad, Geol.).

12. N, arrenvata, L, & H.
M. C., Sydney (J, ¢,).

13. N. pentata, Lesq.
M. C., Sydney (2. Brown).

14. N. Sorzriz (Brongn.).
M. C., Sydney (R. Brown).

15. N. avricunata, Brongn.
M. C., Sydney (2. Brown).

16. N. cyctoprerorpss, spec. nov. Pl. XIII. fig. 94.

Pinnate; pinnules contiguous or overlapping, obliquely round-
ovate, attached at the lower third of the base; nerves numerous,
spreading from the point of attachment. Allied to WN. Vilherse,

Brongn.
M. C., Sydney (#. Brown).

OponrorTERIs, Brongn.

1. Opontopreris ScHLotHEImit, Brongn.
a C. cer (R. Brown) ; Bay de Chaleur (Logan); U.C., Pictou
D.).

CE
2. a SUBCUNEATA, Bunbury.
M. C., Sydney (2. Brown).

156 PROCEEDINGS OF THE GEOLOGICAL society. _[ Dec. 20,

Dictyopteris, Gutb.
DicryoprEeris opLi@vA, Bunbury.
M. C., Sydney (2. Brown).

Loncnorteris, Brongn.
LoNCHOPTERIS TENUIS, spec. nov. Pl. XIII. fig. 103.

Pinnate or bipinnate; pinnules contiguous at the base, nearly at
right angles to petiole, oblong elongate, obtuse. Network of veins
very delicate. Alhed to Z. Bric, Brongn., but with smaller, more
elongate pinnules and finer veins. I suspect this to be a thick-leaved
Pecopteris, showing a coarse cellular reticulation on the upper surface.

M. C., Sydney (2. Brown).

SPHENOPTERIS, Brongn.

1. SpHENOPTERIS MUNDA, spec. nov. Pl. XIII. fig. 97.

Like S. Dubuissonit, Brongn., or S. irregularis, Sternberg, in habit ;
but the pinnules are obovate, decurrent, and few-veined.

M.C., Grand Lake (C. F. Hartt).
2. S. HYMENOPHYLLOIDES, Brongn.

M. C., Sydney (2. Brown); U.C., Joggins (J. W. D.).
3. §. LATIOR, spec. nov. Pl. XIII. fig. 98.

Petiole forking at an obtuse angle, slender, tortuous; divisions
bipinnate; pinne with broad, rounded, confluent pinnules; veins
twice forked, with sori in the forks of the veins. In habit like S.
latifolia, Brongn., S. Newberryi, and S. squamosa, Lesq.

M.C., Grand Lake (C. F. Hartt); U.C., Pictou (J. W. D.).

4, §. pecrprens, Lesquereux.

M. C., Sydney (2. Brown).
5. 8. GRACILIS, Brongn.

M.C., Joggins (J. W. D.); Grand Lake (C. Ff. Harit).
6. S. ARTEMISIHFOLIA, Brongn.

M.C., Grand Lake (C. F. Hartt) ; Sydney (2. Brown).
7. 8. Canapensis, spec.nov. Pl. XIII. fig. 99.

General aspect like S. Haninghausi, but secondary pinnules with
a margined petiole, and oblong pinnules divided into three to five
obtuse points. It is not unlike S. marginata, from the Devonian of
St. John.

Bay de Chaleur (Logan); Sydney ? (2. Brown).
8. 8. Lesquerrvxi, Newberry.

M. C., Sydney (A. Brown).
9, S. mrcrotosa, Guttbier.

M. C., Sydney (R. Brown).

10. S. oprusrtosa (?), Brongn.
M.C., Bay de Chaleur (Logan).

1865. ] DAWSON—COAL-FORMATION, 157

PHYLLOPTERIS, Brongn.
PHYLLOPTERIS ANTIQUA, Spec. noy. Pl. XIII. fig. 96
Pinnate; petiole thick, woody; pinnules oblong, pointed, attached
by the middle of the base; midrib strong, extending to the point, giving
off very oblique nerves, which have obliquely pinnate nervules not
anastomosing. A remarkable frond, which, if not the type of a new

genus, must belong to that above named.

M.C., Sydney (2. Brown).

ALETHOPTERIS, Sternberg.
1. ALETHOPTERIS LONCHITICA, Sternberg.

M. and U. C., Joggins (J. W.D.); M. C., Sydney (4. Brown); Grand
Lake (C. F. Hartt).

Very abundant throughout the Middle and Upper Coal-formations,
and so variable that several species might easily be founded on
detached specimens,

2. A. HETEROPHYLLA, L. & H.
L. C., Parrsborough (A. Gesner).

3. A. Granprni, Brongn.
M. C., Sydney (2. Brown).
4, A, NERVOSA, Brongn.
M.C., el (2. Brown) ; Bay de Chaleur (Logan) ; U.C., Pictou
mn W. D.).
. A. muRicaTA, Brongn.
"an C., Joggins, Bathurst (Lyell); U.C., Pidiou (J. Wy D.).

6. A. prerorpus, Brongn. (A. Brongnartii, Goeppert).
L. or M.C., Bathurst (Lyell’s list).

7. A. Sento, Brongn.
M.C., Sydney (2. Brown); Bay de Chaleur (Logan).

8. A. GRANDIS, spec. nov. Pl. XIII. fig. 100.

Bipinnate ; pinne broad, contiguous, united at the base; veins
numerous, once forked, not quite at right angles to the midrib.
Upper pinne having the pinnules confluent so as to give crenate
edges. Still higher the apex of the frond shows distant decurrent
long pinnules with waved margins. A very large and fine species of
the type of A. Serlu and A. Grandin, but much larger and different
in details. Its texture seems to have been membranaceous; and
fragments from that part of the frond where the long simple pinnules
are passing into the compound ones might be mistaken for an
Odontopteris.

Bay de Chaleur (Logan).

PrcortTeris, Brongn,
1, Prcopreris ARBORESCENS, Schloth.
Seems to have becn an herbaceous species with a very strong

158 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Dec, 20,

petiole. It occurs in an erect position in a sandstone on Wallace
River.

M. C., Sydney (. Brown); U.C., Pictou (J. W. D.); Wallace
River (Dr. Creed). |
2. P. apBReviatTa, Brongn.

M. C., Sydney (2. Brown); Salmon River, U. C., Pictou (J. W. D.).

Very common both in the Upper and Middle Coal-formations.

3. P. RIGIDA, spec. Nov.
Similar to P. arborescens, but much smaller, and with finer nerves.
U.C., Pictou (J. W. D.).

4, P. untta, Brongn.

Certain pinnules of a frond are sometimes swollen as if covered
with fructification below ; and in this state they resemble P. arguta,
Brongn. The sori are seen in other specimens, and are large, round,
and covered with an indusium as in Aspidiwm.

M.C., Sydney (2. Brown); U.C., Pictou (J. W. D.).

5. P. prumosa, Brongn.
M.C., Sydney (2. Brown).

6. P. potymorpHaA, Brongn.
M. C., Sydney (2. Brown).

7. P. acuta, Brongn.
M.C., Pictou (J. W. D.).

8. P. tonerron1A, Brongn.
In Bunbury’s list, from Sydney.

9. P. rHNIOPTEROIDES, Bunbury.
M. C., Sydney (2. Brown).

10. P. cyatuza, Brongn,
M. C., Sydney (#. Brown).

11. P. mquatis, Brongn.
M.C., Sydney (2. Brown).

12. P. Strtmantr?, Brongn.

In Lyell’s list, from Sydney.
138. P. virtosa, Brongn.

M. C., Pictou (Lyeli’s list).
14. P. Bucxtanni, Brongn.

M. C., Sydney (Brown’s list).

15. P. onEOPTEROIDES, Brongn.
M. C., Sydney (Brown’s hist),

1865. | DAWSON—COAL-FORMATION. 159

16. P. pecuRrRENS, Lesq.
Has pinnules more crowded, decreasing towards the apex, but may
be a variety.
_ M.C., Sydney (2. Brown),
17. P. Prucxenett, Sternb.
M. C., Sydney (R. Brown),

Beryertia, Goeppert.
BEINERTIA GaippERTI, spec. nov. Pl. XIII. fig. 101.

Bipinnate ; pinne broad, contiguous, obtuse, with thick pinnules.
Pinnules rounded above, obovate below. Midrib thick, oblique,
dividing above into a tuft of irregular hair-like veins.

M.C., Grand Lake (C. F. Hartt); Bay de Chaleur (Logan); U.C.,
Joggins (J, W. D,).

HYMENOPHYLLITES, Goeppert.
HYMENOPHYLLITES PENTADACTYLA, spec. nov.

In general habit like Sphenopteris microloba, Goepp., but with

pinnules divided into from four to seven obtuse cuneate lobes, each

with one vein.
M. C., Sydney (2. Brown).

Pa.mopTeRis, Geinitz,
1. Patmopreris Harti, spec.noy. Pl. VIII. fig. 35.

Stem or leaf-bases transversely wrinkled with delicate lines ;
sears transversely oval, slightly appendaged below; vascular scars
confluent. Breadth 1:4 in.; length 0°6 in.

M.C., Grand Lake (C. F. Hartt).

2. P. Acapica, spec. nov, Pl, VIII. fig. 36,

Stem or leaf-bases longitudinally striated; scars transverse, flat
above, rounded and bluntly appendaged below; vascular scars in a
transverse row. Breadth of scars 0:7 inch; length 0-5 inch,

U, C., Pictou (J. W. D.).

Caunorreris, L. & H.
Several small erect stems at the Joggins seem to be trunks of ferns,
but are too obscure for description.
Psaronius, Cotta.

Trunks of this kind must be rare in the Nova Scotian coal-fields
A few obscure stems surrounded by cord-like aérial roots haye been
found, and probably are remains of plants of this genus,

Mercapuyton, Artis.
1, MzearuytTon MAGNIFICUM, spec. nov. Pl. VIII. fig. 34.
Stems large, roughly striated longitudinally; scars contiguous,
orbicular, deeply sunk, nearly 3 inches in diameter, and each with a
bilobate vascular impression 2 inches broad and an inch high,

160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

2. M. numize, spec. nov. Pl. VIII. fig. 33.

Stem 2:5 inches in diameter; leaf-scars prominent, flattened, and
broken at the ends, 1 inch wide. Surface of the stem marked with
irregular furrows, and invested with a carbonaceous coating. An
internal axis, nearly 2 inches in diameter, with a coaly coating, sends
off obliquely thick branches to the leaf-scars. This is a very re-
markable specimen, and throws much light on the structure of
Megaphyton. Unfortunately the minute structures are not pre-
served. 3

M. C., Sydney (#. Rrown).

Genus LzprpopEnpRon, Sternberg.

1, LeprpoDENDRON coRRUGATUM, Dawson, Quart. Journ. Geol. Soc.
Vol! xv.) PIT. fie. 05.

Areoles elongate ovate, acute at both ends, with a ridge along
the middle, terminating in a single elevated vascular sear at the
upper end. In certain states the vascular mark appears in the
middle of the areole. In young branches the areoles are contiguous
and resemble those of L. elegans. In old stems they become sepa-
rated by spaces of longitudinally wrinkled bark; in very old stems
- these spaces are much wider than the areoles. Leaves linear, 1 inch
or more in length, usually reflected, one-nerved. Cones (Lepi-
dostrobt) terminal, short, cylindric, with numerous short, acute-tri-
angular scales. Structure of stem :—a central pith with a slender
cylinder of scalariform vessels, exterior to which is a thick cylinder
of cellular tissue and bast fibres, and a dense outer bark.

Var. verticillatum has the areoles arranged in regular decussate
whorls instead of spirally. This difference, which might at first
sight seem to warrant even a generic distinction, is proved by speci-
mens In my possession to be merely a variety of phyllotaais.

This species is eminently characteristic of the Lower Carboni-
ferous Coal-measures, and has not yet been found in the Middle Coal-
formation. Fragments of bark resembling that of this species, occur
in the Coal-formation of Bay de Chaleur, along with leafy branches
of Lepidodendron, which resemble those of this species, though, I
believe, distinct.

L. C., Horton, &e. (C. F. Hartt; J. W.D.); Norton Creek, &c.,
New Brunswick (G. F. Matthew).

2. L. Pictornsz, spec. noy. Pl. IX. fig. 37.

Areoles contiguous, prominent, long oval, acuminate, separated
in young stems by a narrow line; breadth to length as 1 to 3, or
less; lower half obliquely wrinkled, especially at one side. Middle
line indistinct. Leaf-scar at upper end of areole, small, triangular,
with traces of three vascular points, nearly confluent. Length of
areole about 0°5 inch. Leaves contracted at the base, widening
slightly, and gradually contracting to a point; ribs three, central
distinct, lateral obscure; length 1 inch. Cones borne at the ex-
tremities of the smaller branches, oblong, obscurely scaly.

In habit of growth this species resembles Z. elegans, for which

1865. | DAWSON—COAL-FORMATION. 161

imperfect specimens might be mistaken. It is also near to L. binerve
and LZ. patulum, Bunbury*. It abounds in the Middle Coal-measures.
M. C., Sydney (£. Brown) ; Pictou (H.Pooleand J.W.D.); Grand
Lake (C. #. Harit).
3. L. Rrmosum, Sternberg.
M.C., Sydney (2. Brown); Joggins (J. W. D.).
4, L, picuoromum, Sternberg (L. Sternbergit, Ti, Ek).

M. C., arene (R. Brown); Joggins (J. W. D.); L. C., tenet
(J. W. D.).

5. ‘oy DECURTATUM, spec. nov. Pl. IX. fig. 40.

Areoles approximate or separated by a shallow furrow, rhombic

ovate, obliquely acuminate below, nearly as broad as long, wrinkled
transversely, especially on the middle line, which appears tuber-
culated; vascular scar rhombic, twice as broad as long, with three
approximate vascular points. In some flattened specimens the line
separating the areoles is indistinct, and the scars appear on a trans-
versely wrinkled surface without distinct areoles.

M.C., Pictou(J. W. D.).
act, UNDULATUM, Sternberg. Pl, TX. fig. 41.

Possibly several species are included under this name; but they
cannot be separated at present.

M. C., Sydney (R. Brown) ; Joggins and Pictou (J. W. D.); U.C.,
Joggins aa iW. D.).

7. L. prratatum, Lindley & Hutton.

M.C., Joggins (J. W. D.).

8. L., sp. like rerraconum, Goepp.

Obscurely marked, but a distinct species, unless an imperfectly
preserved variety of L. tetragonum. The areoles are square, with a
rhombic scar at the upper corner of each.

L. C., Horton (J. W. D.).

9. L. prnzrve, Bunbury.

M. C., Sydney (2. Brown).

10. L. tumipum, Bunbury,

I think it probable that this species belongs to the genus Lepido-
phloios ; but I have not seen a specimen.
M.C., Sydney (2. Brown).

11. L. eracttz, Brongn.

In Brown’s list in ‘ Ac. Geology.’ Probably a variety of the next.
M. C., Sydney (2. Brown).
12. L.rrneans, Brongn.

In Bunbury and Brown’s lists.
M.C., Sydney (2. Brown).

* Tn certain states of preservation, the lateral ribs of the leaves become obso-

lete; and in others the central disappears, in which state the resemblance to L.
binerve is very close.

162 PROCEEDINGS OF THE GEOLOGICAT, SOCIETY. [Dee. 20,

13. L. prumarium, L. & H.
M. C., Sydney (in Brown’s list).
14. L. sr~acinorss, Sternb.
M. C., Sydney (tn Brown’s list).
15. L. Harcourrm (Witham).
M. C., Sydney (x Brown’s list).
16. L. ctypEatum (?), Lesqx.
M.C., Sydney (2. Brown); U.C., Joggins (J. W. D.).
17. L. acuteatum, Sternberg.
M. C., Sydney (2. Brown).

18. L. pricatrum, spec. nov. Pl. IX. fig. 38.

Leaf-areoles much elongated; breadth to length as 1 to 5 or 6,
transversely rugose; central line indistinct. Leaf-scar rhombic,
with three vascular points; scars in old stems separated by rugose
bark, and somewhat elongate.

M. C., Pictou (J. W. D.).

19. L. pERsonatum, spec. nov. Pl. IX. fig. 39.

Areoles ovate acuminate; breadth to length as 1 to 3 or 4, con-
tiguous in young stems; central lines distinct ; lower part of areole
with transverse lines. Leaf-scars ovate, with two marks above and
two below; leaves slender, 1 inch long, one-nerved.

M.C., Sydney (R. Brown).

HALONIA, sp. Hatonta, L. & H.

A specimen probably referable to this genus from Grand Lake, in
the collection of C. F. Hartt.

Lxprpostrosts, Brongn.

1. Leprpostrosvs vaRriasizis, L. & H.
The most common species.
M. C., Sydney (#. Brown); Pictou and Joggins J. W. Dz).
2. L. sauamosus, spec. nov. Pl. 10. fig. 46.
2 to 3 inches long, 1 inch thick; scales large, broadly trigonal, acute.
Allied toL. trigonolepis, but larger. Probably a cone of Lepidophlovos.
M.C., Grand Lake (C. F’. Hartt).
3. L. LONGIFOLIUS, spec. nov.
Long-leaved, like Lepidodendron longifolium, L. & H.
M.C., Joggins (J. W. D.).
4, LEPIDOSTROBUS, Sp.
Acute trigonal leaves, small.
M. C., Joggins (J. W. D.).
5, LEPIDOSTROBUS, sp.
Round, with obscure scales and remains of long leaves.
L, C., Horton (J. W. D.).

1865.] DAWSON—COAL-=FORMATION. 163

6. L. rrigonoLEPis, Bunbury.

M. C., Sydney (2. Brown).

LxrpmporHytium, Brongn.
1. LeprpopHytium LANnczoLatum, L, & H.
M. C., Joggins; U.C., Pictou (J. W. D.).
2. L. tRINERVE (?), L. & H.

Two-nerved or three-nerved, like D. trinerve, L. & H., but nar-
rower. Both the above are parts of Lepidostrobt.
U.C., Joggins (J. W. D.).

3. L. masus(?), Brongn.
M.C., Sydney (2. Brown).

4, LuprIpoPHYLLUM, sp.

Broad ovate, short, pointed, one-nerved, half an inch long.
U. C., Pictou.

5. L. ivrermepium, L. & H.

M. C., Sydney (#. Brown’s list).

Haloma, Lepidostrobus and Lepidophyllum, including only parts
of Lepidodendron and Lepidophloios, are to be regarded as merely
provisional genera.

Lzrrmopxtoros, Sternberg.

1. LzpmopHioios AcADIANUS, spec. nov. Pl. X. fig. 45, Pl. XI.
fig. 51.

Leaf-bases broadly rhombic, or in old stems regularly rhombic,
prominent, ascending, terminated by very broad rhombic scars
having a central point and two lateral obscure points. Outer bark
laminated or scaly. Surface of inner bark with single points or de-
pressions. Leaves long, linear, with a strong keel on one side, 5
inches or more in length. Cone-scars sparsely scattered on thick
branches, either in two rows or spirally, both modes being some-
times seen on the same branch. Scalariform axis scarcely an inch in
diameter in a stem 5 inches thick. Fruit, an ovate strobile with
numerous acute scales covering small globular spore-cases. This
species is closely allied to Ulodendron majus and Lepidophlowos
laricinus, and presents numerous varieties of marking.

M. C., Joggins, Salmon River, Pictou (J. W. D.); Sydney (&.
Brown).

2. L. PRoMINULUS, spec. nov. Pl. XI. fig. 52.

Leaf-bases rhombic pyramidal, somewhat wrinkled at the sides,
truncated by regularly rhombic scars, each with three approximate
vascular points.

M.C., Joggins (J. W. D.).

3. L. PaRvus, spec.noy. Pl. XI. fig. 50.
_Leaf-bases rhombic, small, with rhombic scars broader than long ;

164 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 20,

vascular points obscure; leaves linear, acute, 3 inches or more in
length, with a keel and two faint lateral'ribs. Cones large, sessile.

U.C., Pictou; M. C., Joggins (J. W. D.); M. C., Sydney (2.
Brown).

4, L, PLATysTIemA, spec.nov. Pl. X. figs. 47 & 48.

Leaf-bases rhombic, broader than long, little prominent; scars
rhombic, oval, acuminate, slightly emarginate above; peo
points two, approximate or confluent.

M.C., Sydney (&. Brown); Joggins (J. W. D.).

5, L. reETRAGONUS, spec. noy. Pl. X. fig. 49.

Leaf-bases square, furrowed on the sides; leaf-scar central, with
apparently a single central vascular point.
M.C., Joggins (J. W. D.).

DipLotEeium, Corda.

DIPLOTEGIUM RETUSUM, Spec. noy. Pl. XIII. fig. 102.

The fragments referable to plants of this genus are imperfect and
obscure. The most distinct show leaf-bases ascending obliquely,
and terminating by a retuse end with a papilla in the notch. Some
less distinct fragments may possibly be imperfectly preserved speci-
mens of Lepidodendron or Lepidophloios.

M. C., Joggins (J. W. D.).

KwoRrRIA.

Nearly all the plants referred to this genus in the Carboniferous
rocks are, as Goeppert has shown, imperfectly preserved stems of
Lepidodendron. In the Lower Coal-formation many such Knorria
forms are afforded by L. corrugatwm.

Kworria Seitoni, Sternberg.

This appears different from the ordinary Knorrie; its supposed
leaves may be aérial roots. It has a large pith-cylinder with very
distant tabular floors, like Sternbergia.

M.C., Sydney (&. Brown). —

Corpaires, Unger. (PycHNoPHYLLUM, rors

1, CorDATTES BORASSIFOLIA, Corda.

M. C., Pictou (4. Poole); Grand Lake (C. F'. Hartt); Sydney
(fh. Brown) ; Jogeins, Onslow (J. W. D.); Bay de Chaleur
(Logan).

Very abundant in the Middle Coal-formation.

2. C, SIMPLEX, spec. nov.

Leaves similar to the last in size and form, but with simple, seals
parallel nerves. It may be a variety, but is characteristic of the
pea Coal-formation.

M.C., Grand River (C.F. Hartt); U.C., Pictou (J. W. D.).

1865. | DAWSON — COAL-FORMATION, 165

Carpiocarpum, Brongn.

1. CaRDIOCARPUM FLUITANS, spec. nov. Pl. XII. fig. 74.
Oval; apex entire or notched; surface slightly rugose ; nucleus
round ovate, acuminate, pitted on the surface, with a raised mesial line.
M. C., Joggins (J. W. D.).
2. C. Bisectum, spec. nov. Pl. XII. fig. 73.
Nucleus as in the last species, but striate ; margin widely notched
at apex, and more narrowly notched below.

M. C., Grand Lake (C. F. Hartt).

3. CarprocaRrpum, sp. like C. marginatum.

M. C., Joggins (J. W. D.).

4, CarpiocarPum, sp. allied to C. latum, Newberry.

M.C., Pictou (4. Poole).

These Cardiocarpa are excessively abundant in the roofs of some
coal-seams; and the typical ones must have been samaras or winged
nutlets. They must have belonged to phznogamous plants, and
certainly are not the fruits of Lepidodendron, though some of the
spore-cases of this genus have been described as Cardiocarpa. These
I propose to place under the provisional genus Sporangites.

SPoRANGITES, Dawson.

1. SPoRANGITES PAPILLATA, spec. nov. Pl, XII. fig. 80.

I propose the provisional generic name of Sporangites for spores
or spore-cases of Lepidodendron, Calamutes, and similar plants, not
referred to the species to which they belong. ‘The present species is
round, about 1 inch in diameter, and covered with minute raised
papille or spines. It abounds in the roof of several of the shaly
coals in the Joggins section, and especially in one in group 19 of that
section.

M. C., Joggins (J. W. D.).
2. S. eLaBra, spec. nov, Pl. XII. fig. 81.

About the size of a mustard-seed, round and smooth. Exceed-
ingly abundant in the Lower Carboniferous Coal-measures of Horton
Bluff, with Lepidedendron corrugatum, to which it possibly belongs.
A similar spore-case, possibly of another species of Lepidodendron,
occurs rarely in the Middle Coal-formation at the Joggins.

STERNBERGIA, Artis.

This provisional genus includes the piths of Dadoxylon, Sigillaria,
and other plants, usually preserved as casts in sandstone, retaining
more or less perfectly the transverse partitions into which the pith-
cylinders of many coal-formation trees became divided in the process
of growth. ‘These fossils are most abundant in the Upper Coal-for-
mation, but occur also in the Middle Coal-formation. The following
varieties may be distinguished :—

(a) Var. approximata, with fine uniform transverse wrinkles. This
is usually invested with a thin coating of structureless coal.

VOL. XXII,—PART I, N

166 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec, 20,

(6) Var. angular, with coarser and more angular transverse
wrinkles. This is the character of the pith of Dadoxylon.

(c) Var. distans, usually of small size, and with distant and irre-
gular wrinkles. This is sometimes invested with wood having the
structure of Calamodendron, and perhaps is not generically distinct
from C. approxvmatum.

d) Var. obscura, with distinct and distant transverse wrinkles,
but not strongly marked on the surface. This is the character of
the pith-cylinders of Sigillaria and Lepidophlovos.

Enpogenttes, L. & H.

Many sandstone-casts, answering to the character of the plants
described under this name by Lindley, occur in the Upper Coal-for-
mation. ‘They are sometimes 3 inches in diameter, and several feet
in length, irregularly striated longitudinally, and invested with coaly
matter. Sometimes they show transverse striation in parts of their
length. I believe they are casts of pith-cylinders of the nature of
Sternbergia, and probably of Sigillarioid trees.

Sorunites, L. & H.

Plants of this kind are found in the sandstones of the Upper Coal-
formation of the Joggins. /

For all the specimens noticed in the above list as collected by Sir
W. E. Logan, Richard Brown, Esq., of Sydney, Cape Breton, Henry
Poole, Esq., of Glace Bay, C.B., and G. F. and C. B. Matthew and
C. F. Hartt, Esqs., St. John, New Brunswick, I am indebted to the
kindness of those gentlemen. To Mr. Brown especially I am under
ereat obligations for his liberality in placing at my disposal his
aa and valuable collection of the plants of the Cape Breton coal-

eld.

EXPLANATION OF PLATES V.-XIIL.
Illustrative of the Coal-plants of British North America.

Prats V.
Fig. 1. Dadoxylon antiquius: longitudinal section, radial, magnified 90 dia-

meters.

2, The same: longitudinal section, tangential, magnified 90 diameters: 4,.
medullary rays.

3. The same: portions of cells showing areolation, magnified 250 dia-
meters.

4. Dadoxylon Acadianum : longitudinal section, radial, magnified 90 dia-
meters.

5. The same: longitudinal section, tangential, magnified 90 diameters: @,
medullary rays.

6. The same: portion of cell showing areolations, magnified 250 dia-
meters.

7. Dadoxylon materiarium: longitudinal section, radial, magnified 70
diameters.

8, The same: longitudinal section, tangential, magnified 70 diameters :
a, medullary rays.

9, The same: portion of cell showing areolation, magnified 250 diameters.

10. D. annulatum: longitudinal section, radial, magnified 70 diameters.

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1865. | - DAWSON—COAL-FORMATION, . 167

Fig.

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Fig.

11. The same: longitudinal section, magnified 90 diameters: a, one of the
concentric rings of compact coaly matter.

12. The same: portion of a cell showing areolation, natural size.

13. Thesame: transverse section, natural size: a, pith; b, wood, composed
of alternate circles of areolated cells and compact coaly matter ; ¢,
coaly bark.

Puate VI.

14. Araucarites gracilis: branch with leaves, three-fourths the natural size.

15. Sigillaria Brownii: portion of two ribs, 4 feet above the level, one-half
the natural size: a, cortical; 6, decorticated.

16. The same: portion of one rib near the root, furrowed and with vascular
scars widely separated.

17. The same: trunk | foot in diameter at the base, showing the origin of
the ribs.

18. The same: photograph of a portion of the upper part of the stem,
one-half the natural size.

19. The same: portion of the base of the stem, one-half the natural size,
from a photograph.

20. The same :: Sigillarian root of this or an allied species.

21. Sigillaria planicosta, from a photograph, one-half the natural size ;
21 a, scar and part of rib, one-half the natural size.

22, catenoides, from a photograph, one-half the natural size ; 22 a, scar
and part of ribs, one-half the natural size.

23 striata : flattened stem, from a photograph, two-thirds the natural
size; 23a, part of stem, same size; 23 0, scar, enlarged.

24. eminens: decorticated stem, from a photograph, much reduced ;
24 a, scar, one-half the natural size.

25, scutellata, from a photograph, two-thirds the natural size, with band
of interrupted growth; 25 a, ordinary areole, natural size; 25 6, are-
oles from the regular band, natural size.

Puate VII.
26. Sigillaria elegans: decorticated stem, from a photograph, one-half the

natural size, with band of interrupted growth at 8; 26 a, corticated
and flattened stem, one-half the natural size, with branches at 6B & y ;
26.6, leaf of S. elegans; 26 c, areoles of a branch; 26 d, areole of
main stem.

27. Bretonensis: corticated stem, from a photograph, two-thirds the
natural size; 27 a, areole, natural size.
28. Sydnensis: decorticated stem, from a photograph, two-thirds the

Fig.

natural size; 28 a, areoles of decorticated stem; 28 & ¢, variety of
Stigmarian root attached to this species.
29. Antholithes squamosus, from a photograph, two-thirds the natural size.

30. Rhabdocarpi, from a photograph, two-thirds the natural size ; 30 a,
a larger specimen of ihe same; 30%, single nutlet of the same,
natural size.

30 ¢. pygmeus: fragment, natural size.

31. Calamodendron approximatum, one-half the natural size; 31 a, cast of
pith; 314, coaly or woody investment; 31 c, tissues of wood of
Calamodendron, magnified,

31d. Tissues of a different species of Calamodendron or of Calamites.

Prats VIII.

32. Leaflets of Cyclopteris Acadica, from a photograph, one-third the na-
tural size; 32a, petiole of the same, one-third natural size; 32,
divisions of petiole, one-half the natural size; 32¢, leaflets; 32 d,
leaflet ; 32 e, leaflet enlarged, showing venation; 32, striation of
petiole enlarged ; 32 g, h, remains of fructification ; 327, base of pe-
tiole, much reduced.

33. Megaphyton humile: B, leaf-scars; y, part of axis: from a photograph,
two-thirds the natural size.

nN 2

168

Fig.

Fig.

Fig.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 20,

34, Megaphyton magnificum: portion of stem, one-sixth the natural size ;
34a, leaf-scar, from a photograph, two-thirds the natural size.
35. Paleopteris Hartii, one-half the natural size.

36. Acadica, one-half the natural size.
Puate IX.
37. Lepidodendron Pictoense, branchlets and leaves, from a photograph,

one-half the natural size (8, cone); 37a, leafy branch; 37 0, branch

with areoles; 37 ¢, larger branch; 37 d, old stem with deep furrows,

and at GB areoles, not enlarged; 37 ¢, leaves. Figs 37a to 37 e, from

photographs two-thirds the natural size. 37/f, areole enlarged; 3749,

leaf enlarged.

plicatum, portion of old stem ; 38 a, areole of branch, these areoles
being placed in contact on such young branches.

39. —— personatum, leafy branch; 39a, larger stem with areoles; both
from photographs, two-thirds the natural size; 39 4, areole, enlarged ;
39 c, leaf, natural size.

38,

40, decurtatum, from a photograph, two-thirds the natural size; 40 a,
areole, enlarged.
41. undulatum, portion of old stem, showing enlarged areoles, fur-

rows, and two cone-scars.
42, 43, Portions of old stems, probably of L. rvmosune or allied species.

Prats X,

. 44, Portions of old stems, probably of Lepidodendron rimoswm or an allied

species.

45. Lesedepilotes Acadianus, stem with marks of cones, from a photograph,
one-half the natural size; 45 a, portion of stem with areoles, from
a photograph, two-thirds the natural size; 45 6, decorticated stem,
natural size; 45¢ & d, opposite sides of the same stem, reduced, to
show the different arrangement of the cone-scars; 45¢e, part of a
leaf, natural size; 45 f, g, h, areoles from different parts of stem.

46. Strobile of Lepidophloios; 46 a, transverse section of a similar strobile ;
from photographs, two-thirds the natural size.

47 & 48. Lepidophlotos platystigma, from a photograph, two-thirds the natural
size; 47 a & 48 a, areole of the same, natural size.

tetragonus, from photograph, two-thirds the natural size; 49a,

areole, two-thirds the natural size.

Puate XI,

50. Lepidophloios parvus, stem with areoles and scars of cones; 50a,
group of leaves ; both from photographs, two-thirds the natural size ;
50 6, areole, natural size.

51. Cross section of Lepidophloios Acadianus, showing the outer rind and
woody axis, one-tenth the natural size; 51 a, scalariform vessels of axis,
magnified ; 51 4, transverse section of part of the axis, showing the
vascular bundles which proceed to the leaves, and the different
diameters of the outer and inner circles of vessels ; 51 c, smaller por-
tion of the axis, showing one bundle of vessels.

. Lepidophloios prominulus, portion of cast, from a photograph, two-
thirds the natural size ; 52a, areole, natural size.

53. Lepidodendron corrugatum, young branch with cone; 53a, branch with
leaves; 53 ¢, older branch with areoles beginning to separate; 53 d,
variety with alternate areoles; 53 ¢, variety with areoles in vertical
rows ; 53 f, g, old trunks, with widely separated areoles; 53 h, pho-
tograph of branch; 537, Kniorriz, or decorticated state; 53 %, frag-
ment, showing ramification ; 53 /, bark with areoles in transverse rows;
53m, spore-case, natural size and magnified; 53” to 7, areoles in
various states; 53s, leaf, enlarged. ;

54. Scalariform vessel of Lepidodendron,

5D. <4 Stigmaria,

49.

On
bo

1865. ] DAWSON—COAL-FORMATION. 169

Puate XII.

Fig. 56. Scalariform vessel of Lepidophloios.
57. Tissues of Sigillaria.
58. Vessel of Sphenophylluim.
59. Tissues of Calamodendron.
60. Tissues of Calamites.
61. Scalariform tissue of Ferns.
62. Bast tissue of Stgillaria.
63. Cells of Dadoxylon Acadianum.
64. Cells of D. materiariwm.
65. Cuticle of Pinnularia.
66. Vessel of Sphenophyllum, 200 diameters.
67. Vessels and cells from vascular bundles of Ferns, 200 diameters.
68. Tissues of Sigzl/aria, 200 diameters.
69. Rhabdocarpusinsignis. . —~ - -
70-72. Cardiocarpum, spp.
73. C. bisectum.
74. C. fluitans.
75. Trigonocarpum minus.
76. T. Stgillarie.
77. T. avellanum.
78. T. intermedium ; 78 a, nucieus of do.
79. T. Neggerathi.
80. Sporangites papillata; 80 b, nat. size.
81. S. glabra; 81 b, nat. size.
82. Fragment of Antholithes.
83. Stigmaria with scars in rhombic areoles.
84. Stigmaria with bark divided by vertical furrows (var. alécrnans),
_ 85. Stigmaria with large scars in elongated areoles.
86. Stigmaria with elongated scars (Cnorria form).
87. Stigmaria another variety, resembling Diplotegiwm.
88. Hguisetites curtus.
89. Calamites Nova-scoticus.

Figs. 54-64 inclusive are drawn to a uniform scale of 90 diameters. Figs. 83 to
87 are taken from photographs, and are two-thirds the natural size.

Puate XIII.

Fig. 90. Asterophyllites trinervis ; 90a, portion of leaf enlarged.
91. Neggerathia dispar, one-half natural size.
92. Cyclopteris hispida; 92a, portion of pinnule magnified, showing hairy
surface and impressions of nervures.

93. Newropteris perelegans; a, portion magnified, showing venation.

cyclopteroides.

95. Cyclopteris antiqua.

96. Phyllopteris antiqua; 96 a, portion magnified, showing venation.

97. Sphenopteris munda; 97 a, portion magnified.

latior ; 98 a, pinnule magnified, showing venation and sori.

99. Canadensis; 99 a, pinnule magnified, showing venation.

100 and 100a & d. Pinnules of Alethopteris grandis; 100 a, portion mag-
nified, showing venation.

101. Beinertia Goepperti; 101 a, pinnule magnified, showing venation.

102. Diplotegium retusum; 102 a, leaf-scar magnified.

103. Lonchopteris tenuis; 103 a, portion enlarged, showing character of sur-
face.

‘Se

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From October 1st to December 31st, 1865.

I. TRANSACTIONS AND JOURNALS.

Presented by the respective Societies and Editors.

American Philosophical Society. Proceedings. Vol. x. No. 73.

P. W. Sheafer.—Relative Levels of Coal- and Oil-regions, 32.
J. P. Lesley.—Petroleum of Kentucky, 33 (2 plates).

Anglo-Brazilian Times. Annol. No.18. October 24,1865. From
the late G. H. Roberts, Hsq., F.GS.

Anthropological Review. Vol.in. No.11. October 1865.
Assurance Magazine. Vol. xii. Part 5. October 1865...

Atheneum Journal. Nos. 1980-1992. October to December 1865.

Notices of Meetings of Scientific Societies, &c.

The Stone Age, 469, 736.

Meeting of British Association, A71, 506.

T. Austin’s ‘ Millstone Grit and its Fossils,’ noticed, 501.

J.W. Salter and H. Woodward’s ‘ Chart of Fossil Crustacea,’ noticed,
371.

G. Greenwood.—Arnott versus Murchison, 621.

Petroleum in Canada, 698.

ee Field-Naturalists’ Club. Reports for 1863-64 and 1864-65.
rom R. Tate, Esq., F.GS.

Berlin. Zeitschrift der deutschen geologischen Gesellschaft. Vol. xvii.
Heft 2. February to April 1865.

F. Roemer.—Ueber das Vorkommen von Rhizodus Hibberti, Owen
(Megalichthys Hibberti, Agassiz et Hibbert), in den Schieferthonen
des Steinkohlengebirges yon Volpersdorf in der Grafschaft Glatz,
272 (plate).

DONATIONS. 171

Berlin. Zeitschrift der deutschen geologischen Gesellschaft. Vol. xiv.
Heft 2 (continued).

G. vom Rath.— Hin Besuch der Kupfergrube Monte Catini in Toscana
und einiger Punkte ihrer Umgebung, 277 (2 plates).

A. Kunth.—Die losen Versteinerungen im Diluvium von Tempelhof
bei Berlin, 311 (plate).

H. Hofer.—Tertiarconglomerat im Trachyte zu Nagyag, 333.

K. v. Seebach.—Beitrage zur Geologie der Insel Bornholm, 338

(plate).

Webshy. Ueber Quarz-Krystalle von Striegau in Schlesien, 348

late).

R. ae dem thiiringischen Schiefergebirge, 361 (2 plates).

O. von Albert.—Darstellung der geognostischen Verhaltnisse der
Braunkohlen-Ablagerung bei Latdorf in Anhalt, 377 (plate).

F. A. Roemer.—Bemerkungen tber die geognostische Colorirung der
Karte des westlichen Harzgebirges, 388.

H. Credner.—Geognostische Skizze der Umgegend von New York,
388.

G. vom Rath.—EHin Besuch Radicofani’s und des Monte Amiata in
Toscana, 399 (plate).

Bombay. Geographical Society. Vol. xvii. 1863-64. 1865.
C. Dodd.—Island rising out of the Sea, 233.
D. J. Kennelly.—EKarthquake in the North-western part of the
Bombay Presidency, 288.

Boston Society of Natural History. Conditions and doings as exhi-
bited by the Annual Reports, May 1865.

Calcutta. Asiatic Society of Bengal. Journal. Part II. No. 2. 1865.
H. B. Medlicott.—Notes on the Sivalik Fauna, 63.
H. H. Godwin-Austen.—On the Sandstone formation, &c., near Buxa
Fort, Bhootan Dooars, 106 (plate).

Canadian Journal. NewSeries. Vol.x. No.59. September 1865,

Canadian Naturalist and Geologist. Vol.u. No.4. August 1865.

T. MacFarlane.—Extraction of Copper from its Ores in the Humid
Way. Part 2, 241.
——. Geological Sketch of the Neighbourhood of Rossie, 267.
&— T.S. Hunt.—Chemistry of Mineral Waters. Part 3., 276.
J. F. Whiteaves.—Fossils of the Trenton Limestone of the Island of
Montreal, 312.
‘Geology of New Brunswick,’ part i1., noticed, 314.

Chemical Society. Journal. Second Series. Vol.ii. Nos. 33-35.
September to November 1865.

A. H. Chureh.—Chemical Researches on some new and rare Cornish
Minerals, 259.

Colliery Guardian. Vol. x. Nos. 249-261. October to December
1865.
Bone-cave at Ryhope Colliery, 288.

North of England Institute of Mining Engineers, 289.
Mineral lands of Illinois, 294.

172 . DONATIONS.

Colliery Guardian. Vol. x. Nos. 249-261 (continued).

Lake Superior iron, 295.

New Jersey iron-ore mines, 296.

Dudley and Midland Geological Society, 296.
Coal-mining in Bohemia, 549.

Coal-fields of Mold and its vicinity, 354.
Lackawanna Coal-field, 356.

Discovery of coal at Winscombe, 369,

Dudley Geological Society, 373.

Hematite deposits in Pembrokeshire, 376.
Discovery of lead in the Forest of Bowland, 376.
Titaniferous iron-sand of New Zealand, 390,
Schuylkill Coal-field, 392.

Geological Society of London, 892, 431, 472.
Coal-fields of Hawarden and Buckley, 393.
Mineral-field of Southern Illinois, 394.
Gold-mining in New Zealand, 396.
Coal-discovery in Victoria, 414. —

Mount Diablo Coal-mines, 415.

Manchester Geological Society, 481, 513.
Tron and coal in Ohio, 496.

South Wales Institute of Mining Engineers, 516.

Copenhagen. Oversigt over det Kongelige danske Videnskaberncs
Selskabs Forhandlinger. 1864.

Forchhammer.—Om Aidelforsit og nogle andre dertil horende Mine-
ralier, 64.

Det saakaldte Kalktrisilicat fra Gjellebek ved Drammen i
Norge, 71.

. Den parallel-traadige eller asbestagtige Okenit fra Nordgr@n-

land, 73.

Edinburgh. Royal Society. Proceedings. Vol.v. No. 65. 1864-65.

——. -——. Transactions. Vol. xxiv. Part 1. 1864-65.
W. L. Lindsay.—Tertiary Coals of New Zealand, 167.

Geneva. Mémoires de la Société de Physique et @’Histoire Natur elle.
Voloxvim.” I"* partie: ise5.

P. de Loriol et A. Jaccard.—Etude géologique et paléontologique de
la formation d’eau douce infra-crétacée du Jura, et en particulier
de Villiers-le-Lac, 63 (5 plates).

Geological Magazine. Vol. 1. Nos. 16-18. October to December
1865.

W. Carruthers.—Undescribed Cone from the Carboniferous Beds of
Airdrie, Lanarkshire, 438 (plate).

A. H. Green.—Supposed Ice-scratches in Derbyshire, 440.

G. H. Kinahan. Te Preclacial (?) Drift in Queen’s County, 442.

a: Haughton’s ‘Manual of Geology,’ noticed, 449.

G. F. Browne’s ‘Ice-caves of France and Switzerland,’ noticed, 449.

G. Burmeister’s ‘Annals of the Museum of Buenos Ayres,’ noticed,
451.

N. Whitley’s ‘ Flint Implements from Drift, not authentic,’ noticed,
455.

DONATIONS. 173

Geological Magazine. Vol. ii. Nos. 16-18 (continued).

W. B. Dawkins.—Paleontology of the Rheetic (Penarth) Beds in
Western and Central Somerset, 481.

W. Carruthers.— Caulopteris punctata, Goepp., a tree fern from the
Upper Greensand of Shaftesbury in Dorsetshire, 484 (plate).

A. L, Adams.—History of the Discovery of the F ossil Elephant of
Malta, 488.

T. Harrison.—Geology of Hobart Town, 491.

D. Mackintosh.—Notes on Charnwood Forest, 498.

R. B. Foote’s ‘Occurrence of Stone Implements in Lateritic For-

mations in various parts of Madras and North Arcot Districts,’
noticed, 503.

i Codrington’s ‘Geology of the Berks and Hants Extension and
Marlborough Railways,’ noticed, 504,

H. Seeley.— Section discovering the Cretaceous Beds at Ely, 529.

G. E. Roberts —Rocks and Minerals of Finlan d, 554.

F, E. Edwards.—New Eocene Species of Cyprea and Marginella, 536

late).

Bi i eadiey -Tracks in the Manx Slates, 542.

W. K. Parker and T. R. Jones’s ‘Foraminifera from the North
Atlantic and Arctic Oceans, including Davis’s Straits and Baflin’s
Bay,’ noticed, 548.

W.S. Jevons’s “ Coal Question: an Inquiry concerning the Progress
of the Nation and the probable Exhaustion of cur Coal-mines,’
noticed, 550.

T. Austin’s ‘ Millstone Grit, its Fossils, &c.,’ noticed, 552.

G. C. Haswell’s ‘Silurian Formation in the Pentland Hills,’ noticed,
553. ;

T. C. Winkler’s ‘Musée Zeyler. Catalogue Systématique de la Col-
lection Paléontologique,’ noticed, 555.

Notices of British and loreign Memoirs, 444, 501, 544.

Reports and Proceedings, 456, 508.

Correspondence, 471, 520.

Miscellaneous, 478, 528.

Geological and Natural History Repertory. Vol.i. Nos. 6-8. Qc-
tober to December 1865.

Meeting of British Association, 141.

J. Lubbock’s ‘ Prehistoric Times,’ noticed, 85.

S. J. Mackie.—Summer Rambles—A day at Aldington and Court-
at-street, 111.

R. Tate. — Descriptive catalogue of the Pteroceree of the Cretaceous
Rocks, 91.

Proceedings of Societies, 201.

Correspondence, 201.

Giessen. Elfter Bericht Ger Oberhessischen Gesellschaft fiir Natur-
und Heilkunde. 1865.

Glasgow Geological Society. Proceedings. Vol. ii. Part 1. 1865.

A. Geikie.—Origin of the Present Scenery of Scotland, 4.

J. Young.—New Chiton and new Chitonellus from the Carboniferous
Rocks of Western Scotland, 13.

J. Thomson —On a Chiton plate and Entomostraca, 15.

174 DONATIONS,

Glasgow Geological Society. Proceedings. Vol. ii. Part 1 (continued).

J. Russell.—Reptilian-remains from black-band ironstone, Airdrie,

J. Bryce.—Age of certain Trap-Rocks in the neighbourhood of
Glasgow, 17.

H. W. Crosskey.—Section near Inch-na-Damff, 19.

A. T. Machattie—On Metamorphism, with special reference to
Chemical Changes in Rocks, 20.

J. Armstronge.—Two new species of Cypricardia from the Carbo-
niferous Limestone of Lanarkshire, 28.

A. Armour.—Fish-remains from Cambuslang, 29.

J. Dougall.—Ancient Sea-margins around Glasgow, 30.

J. Young.—Peculiar varieties of Old Red and Carboniferous Sand-
stones from near Glasgow, 33.

J. W. Young.—Analysis of Ferrite, anew red mineral from Paisley, 36.

J. Young.—Occurrence of Rhizodus Hibberti in Carboniferous Strata
near Glasgow, 38.

J. Reid.—Continuous internal movements in the earth’s crust, 40.

R. W. Skipsey.—Position and Character of several of the Igneous
Rocks and Minerals in the northern front of the Cathkin Hills, 41.

H. W. Crosskey.—Glacial-deposits of the Clyde District, 45.

R. W. Skipsey.—Discovery of Carboniferous Limestone Fossils in
the Upper Coal-measures to the east of Glasgow, 52.

J. D. Campbell.—Results of the Ice-action in Scotland and Switzer-
land, 54.

J. Sutherland.—Quartz and its mode of formation, 56.

G. Somerville—Geological Features of the Country around Jeru-
salem, 61.

J. W. Young.—Presence of Magnesia in Rocks, 64.

J. Bryce.—Harthquake District of the County of Perth, 70.

T. R. Jones.—New species of Estherta from the Carboniferous Lime-
stone of Thornlierank, Renfrewshire, 71.

J. Young.—Estheria punctatella, 72.

J. Armstrong.—Discovery of the Teeth of Dithyrocaris, 73.

——. Two new species of Shells from the Carboniferous Limestone

of Clydesdale, 74. |

J. Thomson.—Geology of Campbeltown District, 76 (plate).

J. W. Young.—Analysis of Minerals from Campbeltown, 89.

H. W. Crosskey.—Address, 90.

Heidelberg. Verhandlungen des naturhistorisch-medizinischen Ver-
eins: |. Volvay. 4) No. a1 865;

C. W. C. Fuchs.—Ueber die Entstehung einiger Mineralien, 16.

Institution of Civil Engineers. Abstracts of Proceedings. Nos. 1
& 3. Session 1865-66:

Intellectual Observer. Vol. viii. Nos. 45-47. October to December
1865.

Notices of Meetings of Scientific Societies, &e.

S. Haughton’s ‘Manual of Geology,’ noticed, 199.

H. Emanuel’s ‘Diamonds and Precious Stones,’ noticed, 216.

Meeting of the British Association, 236.

Glace Ae Crustacea (Recent and Fossil), 821
plate).

TM Tl—Flint Tools of North Devon, 350 (2 plates).

DONATIONS. 175

Iinnean Society. Journal of Proceedings. Vol.vili. Nos. 31 & 32.
1865.

London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xxx. Nos. 203-205. October to December 1865.
From Dr. W. Francs, F.GLS.

J. Prestwich.—Raised Beach of Sangatte, &c., 378.

C. Le N. Foster and W. Topley.—Superficial Deposits of the Medway

and Denudation of the Weald, 379.

E. Lartét.—On Ovibos moschatus, Blainville, 379.

J. W. Salter.—Additional Fossils from the Lingula-flags, 380.

H. Woodward.—New genus of Cirripedia in the Wenlock Shale of
Dudley, 380.

—. New species of Eurypterida, 380.

. New genus of Hwrypterida from the Lower Ludlow Rocks of
Leintwardine, Shropshire, 381.

H. Godwin-Austen.—Carboniferous Rocks of Kashmere, 381.

W. B. Dawkins.— Mammalian Remains found by E. Wood, Esq., near
Richmond, Yorkshire, 382.

J. Tyndall.—Professor Helmholtz on Ice and Glaciers, 393.

R. A. C. Godwin-Austen.—Submarine Forest-beds in Porlock Bay,
452.

R. B. Watson.—Marine Origin of the “ Parallel Roads” of Glen Roy,
452.

London Review. Vol. xi. Nos. 275-287. October to December
1865.

Notices of Meetings of Scientific Societies, &c.
‘Frost and Fire,’ noticed, 415.
R. M. G. Browne’s ‘ Astronomical Geology,’ noticed, 700.

Manchester Geological Society. Vol.v. Nos. 8-11. 1864-65. -

Brequet.—Dumas’ Lamp, for the use of miners, 131.
J. J. Horsfall.—Pit-head frames, 142 (4 plates).
EK. W. Binney.—Objects of the Manchester Geological Society, 158.

Matériaux pour Vhistoire positive et philosophique de Homme.
2° Année. September 1865. From M. G. de Mortillet.

Delesse et Laugel’s ‘Revue de Géologie pour les années 1862 et
1863,’ noticed, 9.

P. Strobel et L. Pigorini’s ‘Le Terremare e le palafitte del Par-
mense, seconda relazione,’ noticed, 14.

L, Pigorini’s ‘Le abitazioni di Fontanellato dell’ epoca del ferro,’
noticed, 21. ;

‘Palafitta sopra terra ud all’ ascietto di Castellazzo di Fonta-

nellato,’ noticed, 24. A

J. Lubbock’s ‘ Pre-historic Times, as illustrated by ancient remains
and the manners and customs of modern savages,’ noticed, 25.

A. Milne-Edwards’s ‘ Faune ornithologique de l’époque quaternaire,’
noticed, 25.

J. Delanoue’s ‘ Habitations lacustres dans l’intérieur de la France,’
noticed, 28.

Bourgeois’s ‘ Note sur le diluvium de Vendéme,’ noticed, 29.

D’Archiac’s ‘Note sur l’existence de restes organiques dans les
roches laurentiennes du Canada,’ noticed, 31.

176 DONATIONS.

Matériaux pour Vhistoire positive et philosophique de Homme.
2° Année. September 1865 (continued).

V. Meunier’s ‘ La science et les savants en 1865,’ noticed, 33.

HE. Robert’s ‘Nouvelles observations critiques sur la prétendue co-
existence de l’Homme avec les grandes espéces éteintes de pachy- -
dermes, ainsi que sur l’age de pierre,’ noticed, 37.

Bourgeois.—Poignard en silex trouvé a Pontlevoy, 41.

G. Ramorino.—Ossements pliocénes avec diverses impressions, 41.

J. B. Noulet’s ‘Fossiles et cailloux travaillés des dépéts quaternaires

_ de Clermont et de Venerque,’ noticed, 42.

Lartet.—Lame (ivoire fossile trouvée dans* un gisement ossifére du-
Périgord, et portant des incisions qui paraissent constituer la re-
production d’un Kléphant a longue criniére, 46.

De Vibraye.—Sur la reproduction en bois de Renne d’une téte (pré-
sumée) de Mammouth et sur quelques morceaux d’ivoire travaillé
provenant plus particuliérement des stations du Périgord, 49,

Laube.—Apparition et disparition des formes animales, 56.

Guyon.—Origine des Kabyles ou Berberes, 57.

Charvet.—Exposition antéhistorique, 57.

Medical Press. Second Series. Vol. xu. No. 303. October 11,
1865.

Melbourne. Royal Society of Victoria. Transactions. Vol.vi. 1861—
64. 1865.

J, E. Woods.—Tertiary Fossils of South Australia, 3.

T. S. Ralph.—Drysodil from Tasmania, 7.

F. McCoy.—Dzwprotodon, 25.

W. B. Clarke.—Coal-seams near Stony Creek, West Maitland Dis-
[seria 21

. Geology of the Maranoa District, 32.

F, McCoy.—Fossils from Wollumbilla, 42.

H. Watts.—Fossil Polyzoa, 82.

T. Harrison.—Geology of Hobart Town, 131.

Moscow. Bulletin de la Société Imperiale des Naturalistes. Vol.
xxxvil. Nos. 2-4. 1864.

H. Romanowsky.— Description de quelques restes de poissons fossiles,
trouvés dans le calcaire carbonifére du gouvernement de Toula,
157 (2 plates).

V ol sexxyatey SNos li eGo:

H. Trautschold.—Der Inoceramen-Thon von Ssimbirsk, 1.
Handrikoff.—Solution d’un probléme fondamental de Géodésie, 246.

Vol. xxxvii. No.2. 1865.

R. Hermann.—Ueber die Zusammensetzung von Wohlerit, Aeschy-
nit, und Euxenit, sowie Bemerkungen iiber Zirkonerde, 465.

oe
.

Munich. Sitzungsberichte der kénigl.-bayer. Akademie der Wissen-
schaften. Vol. iu. Hefte 1&2. 1865.

V. Kobell.—Ueber einen Brochantit aus Chile, 70.

New York. American Geographical and Statistical Society. Vol. ii.
Nos.3 & 4. 1863-64.

DONATIONS. LF

Nova Scotian Institute of Natural Science. Proceedings and Trans-
actions. Vol. ii. Part 3. 1864-65,

W. Gossip.—Antiquity of Man, 80.

H. How.—Economic Mineralogy of Nova Scotia. Part ii. Ores of
Manganese and their Uses, 128.

Contorted Quartz at Laidlaw’s “ Diggins,” 142.

Padova. Rivista Periodica dei Lavori della I.R. Accademia di Scienze,
Lettere et Arti. Vol.i. Nos. 1-4. 1851-53.
Marchand.—Sulle acque naturali e loro origine geologica, 29.

De Zigno.—Sui terreni jurassici delle Alpi venete, 187.
. Sulle Cicadee fossili delle Oolite, 345.

—. ——. Voli. Nos.5&6. 1853-54.
—. . Vol. in. Nos.7&8. 1854-55,

De Zigno.—Sulle ossa fossili di Rinoceronte, trovate in Italia, 116.
—. . Vol.iv. Nos.9&10. 1855-56.

Massalongo.—Descrizione di alcuni Fuchi fossili della Calcaria del
Monte Spilecco nella Provincia Veronese, 207 (6 plates).

—. . Vol.v. Nos.11 &12. 1856-57,
De Zigno.—Sui resti fossili dei pesci trovati nel Veneto, 21.
—. wv Ol. Vi. Nos. 13. & 14... 1857-58.

Ronconi.—Delle probabili condizioni fisico-dinamiche, le quali pos-
sono avere accompagnato nelle epoche geologiche la solidificazione
delle sostanze organiche e vegetali. Part 1., 59.

Vol. vn. Nos: 15°& 16, 1858-59.

De Zigno.—Delle Alghe e delle Calamarie dei terreni oolitici, 97.
Molin.—Della Collezione dei pesci fossili di monte Bolca, conservati
nel Gabinetto della I.R. Universita di Padova, 261.

ee. Vol. vil. Nos. 1/7 & 18. 1859-60:
Vol. ix. Nos. 19 & 20. 1860-61.

De Zigno.—Cenni sulla costituzione geclogica dei Monti Euganei, 93.
——. ——. Vol.x. Nos. 21 & 22. 1861-62.
Vol. xu. Nos. 23 & 24. 1862-63.

De Zigno.—Sopra i depositi di piante fossili dell’ America settentrio-
nale, delle Indie e dell’ australia che alcuni autori riferirono all’
epoca oolitica, 139.

ae) Vol. xii. Nos, 25.6 262..1863-_64.

—
e

ooo

Palermo. Giornale di Scienze Naturali ed Economiche. Vol. i.
Fase. 2: 1865.

G. G. Gemmellaro.—Nota sopra una Spherulites del turoniano di
Sicilia, 151 (plate).

178 DONATIONS,

Paris. Bulletin de la Société Géologique de France. Deuxiéme
Série. Vol. xxii. Feuilles 17-26. 1865.

L. Pareto.—Sur les subdivisions que l’on pourrait établir dans les
terrains tertiaires de l’Apennin septentrional, 257.

L. Vaillant.—Sur la constitution géologique de quelques terrains aux
environs de Suez, 277 (plate).

EK. Dumortier.—Fossiles découverts dans un gisement a Lyon
(Rhone), 287.

J. Marcou.—Le Niagara quinze ans aprés, 290 (plate).

Em. Benoit.—Sur les ablations et dépdts superficiels antérieurs a
V’époque quaternaire dans le Jura méridional, 300.

G. de Mortillet.—Age des débris d’Elephas primigenius trouvés prés
de Tenay (Ain), 305.

A. Boué.—Approvisionnement d’eau pour Vienne (Autriche), 309.

H. Renevier.—Géologie du massif de l’Oldenhorn et du col du Pillon,
514.

Virlet d’Aoust.—Sur une faune pyrénéenne nouvelle des lignites
mioceénes d’Orignac (Hautes-Pyrénées).—Ophites des environs de
Bagnéres-de-Bigorre, etc., 318.

Ed. Lartet.—Sur une dent molaire et une portion de crane d’ Ovibos
moschatus, 354.

Ch. Martins.—Le Spitzberg.—Tableau d’un archipel 4 V’époque gla-
ciaire, 336.

EK. Desor.—Sur la disposition des massifs cristallins des Alpes ou
zones d’affleurement, 354 (plate).

A. Leymerie.—Sur l’étage garumnien, 360.

J. Martin.—Etage rheetien a Avicula contorta, etc., 369.

F, Garrigou.—Etude comparative des alluvions quaternaires anciennes

et des cavernes 4 ossements des Pyrénées, 396.

G. de Mortillet.—L’industrie des pierres a fusil et les silex taillés du
Grand-Pressigny, 402.

L’abbé Lambert.—Découverte d’une bréche osseuse dans le caleaire
grossier inférieur 4 Trosly-Loire (Aisne), 404.

A. Damour.—Sur un hydrate d’alumine ferrugineuse trouvé dans l’ile
d’Egine (Gréce), 415.

Photographic Journal. Vol.x. Nos.162-164. October to December
1865.

Prague. Erster Jahres-Bericht tiber die Wirksamkeit der beiden
Comitiés fiir die naturwissenschaftliche Durchforschung von Boeh-
men im Jahre 1864. 1865.

Quarterly Journal of Microscopical Science. Vol. xii. No.20. Oc-
tober 1865.

Quarterly Journal of Science. Vol. ii. No. 8. October 1865.

H. M. Jenkins.—Strata identified by Organic Remains, 622 (plate).

R. Hunt.—British Gold, 635. ,

Chronicles of Science, 644.

Meeting of British Association, 727.

D. T. Ansted.—Petroleum-springs of the Crimea and Shores of the
Sea of Azof, 755.

DONATIONS. 179

Reader. Vol. vi. Nos. 145-157. October to December 1865.

Notices of Meetings of Scientific Societies, &c.

Meeting of British Association, 406, 434, 463, 490, 519, 546.

O. Fisher.—The Glacial Submergence, 410, 521.

J. Croll.—Physical Cause of the Submergence of the Land during
the Glacial Epoch, 435.

H. Pratt.—The Glacial Submergence, 486.

Quartz and Felspar, 462. :

S. V. Wood, jun.—On the Glacial Submergence, 465.

J.W. Salter and H.Woodward’s ‘Chart of Fossil Crustacea,’ noticed,
545, 7

J. Croll.—The Glacial Submergence, 630, 659.

Royal Astronomical Society. Memoirs. Vol. xxxii. Session 1863-
64. 1865.

Royal Horticultural Society. Proceedings. Vol.v. No.8. August
to November 1865.

Royal Institution. Proceedings. Vol. iv. Parts 5 & 6. 1865.

A. C. Ramsay.—The Hozoon and the Laurentian Rocks of Canada
374,

Royal Irish Academy. Proceedings. Vol. ix. Part 1. 1865.
——. Transactions. Vol. xxiv. Polite Literature. Part 2. 1865.
Vol. xxiv. Scvence. Parts 4&6. 1865.

——, ——, Vol. xxiv. Antiquities. Parts 2-4. 1864-65.
Royal Society. Proceedings. Vol. xiv. No. 78. 1865.

St. Petersburg. Académie Impériale des Sciences. Bulletin. Vol.vii.
Nos. 3-6. 1864.

P. Sémionof et V. Moller.—Sur les couches devoniennes supérieures
de la Russie centrale, 227 (4 plates).

N. Kokcharof.—Mesures d’un cristal particuliérement régulier de
Vanorthit du Vésuve, 326.

J. F. Brandt.—Découverte de deux molaires d’Elasmotherium au
gouvernement de Saratof, 352.

Duc N. de Leuchtenberg.—Sur la composition du pyrite magnétique
de Bodenmais, 403.

N. Kokcharof.—Sur le Lépolithe, 405.

M. Pusyrewsky.—Le minerai de fer provenant du puits artésien de
St. Pétersbourg, 474.

J. F. Brandt.—Sur les restes trouvés jusqu’a présent de |’ Hlasmothe-
rium, 480.

a... Vol. vis: Nos. 126") 1864,

A. de Volborth.—Sur le Baerocrinus, une nouvelle espéce de crinoide,
trouvée en Hsthonie, 177 (plate).

M. Helmersen.—Le puits artésien 4 St. Pétershourg, 185 (plate).

F., Schmidt.—Recherches sur les phénoménes produits par la période
de glaces en Esthonie et a Vile d’Oesel, 339 (plate).

N. Kokcharof.—Notice sur le pyroxéne russe, 371.

H. Moritz.—Les tremblements de terre dans la Caucasie, 384.

G. de Helmersen.—Le bassin houillier de Donetz, et son avenir in-
dustriel, 465,

—S oe

180 DONATIONS.

St. Petersburg. Académie Impériale des Sciences. Mémoires. Vol. v.
Now 1. "Sez.

——. Vol.vii. Nos.1-9. 1863-64.
N. v. Kokscharow.—Ueber den Lepolith.

eg Aol am, NOR, =

J. F’, Brandt.—Observations de Elasmotherw reliquiis (6 plates).

N. v. Kokscharow.—Notiz wber den Chiolith.

A. von Volborth.—Ueber einige neue esthandische Illzenen (2 plates).

H. Struve.—Die artesischen Wasser und untersilurischen Thone zu
St. Petersburg.

N. v. Kokscharow.—Beschreibung einiger Topas-krystalle.

——. Monographie des Russischen Pyroxens (5 plates).

Society of Arts. Journal. Vol. xiii. Nos. 672-677. October and
November 1865.
Notices of Meetings of Scientific Societies, &e.
Meeting of British Association, 730.

——, ——. Vol.xiv. Nos. 678-684. November and December
1865,

J. B. Denton.— Water-supply, 17.
Copper-mines in New South ai 65.

Sydney Morning Herald. Vol. lii. No. 8517. September 7, 1865.
From W. Keene, Esq., F'.GLS.

W. Keene.—Petroleum Coal-seams, 5.

Tasmania. Royal Society. Monthly Notices of Papers and Pro-
ceedings. 1863.

T. Stephens.—Coal-seam at Mangana.
B. R. Chesney.— Volcanic Action in New Zealand (map).

——, ——. ——. 1864.
S. i. Wintle.—Post-Tertiary Shell-deposits around Hobart Town, 32.
——. -—-—. Reports for 1863 and 1864.

Vienna. Kaiserliche Akademie der Wissenschaften. Abstracts of
Proceedings. Nos. 21-26. 1865.
Peters.—Aus den tertiairen und secundiren Schichten der Dobrudscha,
15},
A. E. Reuss.—Die Foraminiferen und Ostracoden der Kreide am
Kanara-See bei Kustendsche, 167.
A. Boué.—Ueber das Zusammentreffen fossiler Ueberbleibsel aus
mehreren Classen der organischen Welt, 182.

——, Sitzungsberichte der kaiserlichen Akademie der Wissenschaf-
ten. Mathematisch-naturwissenschaftliche Classe. Vol.1. Erste
Abtheilung. Hefte 2-5. 1864-65.

Reuss.—Ueber einige Anthozoen der Késsener Schichten und der
alpinen Trias, 153 (4 plates).
. Ueber Anthozoen und Bryozoen des Mainzer Tertiirbeckens,
197 (3 plates).

DONATIONS. 181

Vienna. Sitzungsberichte der kaiserlichen Akademie der Wissen-
schaften. Mathematisch-naturwissenschaftliche Classe. Vol. 1.
Erste Abtheilung. Hefte 2-5 (continued).

Peters.—Vorlaufiger Bericht tiber eine geologische Untersuchung der
Dobrudscha, 228.

Laube.—Die Fauna der Schichten von St. Cassian. Ein Beitrag zur
Palaontologie der alpinen Trias, 319.

VY. Zepharovich.— Die Anglesit-Krystalle von Schwarzenbach und
Miss in Karnten, 369 (plate).

Tschermak.—Chemisch-mineralogische Studien. I. Die Feldspath-
eruppe, 566 (2 plates).

Reuss.—Zur Fauna des deutschen Oberoligociins, II. Abtheilung,
614 (10 plates).

Karrer.—Ueber das Auftreten der Foraminiferen in den Mergeln der
marinen Uferbildungen (Leythakalk) des Wiener Beckens, 692
(2 plates).

—

—. . ——. Vol. 1. Zweite Abtheilung. Hefte 1-5.

1864-65,

HE. Ludwig.—Chemische Analyse der Mineralquellen von Johannis-
brunn in Mihren, 247,

Schrotter.—Ueber ein vereinfachtes Verfahren, das Lithium, Rubi-
dium, Casium und Thallium aus den Lithionglimmern zu gewinnen,
268.

Haidinger.—Ein yorhomerischer Fall von zwei Meteoreisenmassen
bei Troja, 288. —

Ditscheiner.—Die Krystallformen einiger Platincyanverbindungen,
373 (plate).

Haidinger.—Der Meteorsteinfall von Polinos in den Kykladen, 458.

—. —. . Vol. li. Erste Abtheilung. Hefte 1 & 2.
January and February 1865.

Boué.—Bibliographie der kiinstlichen Mineralienerzeugung, 7.

R. v. Zepharovich.— Ueber Bournonit, Malachit und Korynit von Olsa
in Karnten, 102.

Tschermak.—Chemisch-mineralogische Studien, II. Kupfersalze,
127.

Boué.—Ueber den wahrscheinlichen Ursprung des menschlichen
Geschlechtes, nach den jetzigen naturhistorischen Kenntnissen, so
wie auch iiber den palaontologischen Menschen, 142.

——. Vol. li. Zweite Abtheilung. Hefte 1 & 2.

1865.
Loschmidt.—Krystallbestimmungen einiger Oxalsaure-Verbindun-
gen, 7 (plate).
V. Hauer.—Ueber die Gliederung der oberen Trias der lombardischen
Alpen, 33,

. Verhandlungen der k.-k. geologischen Reichsanstalt. Vol. xv.
Heft 4. 1865.

Ansprache des Directors, 213.

VOL. XXII,—PART I, 0

te2 DONATIONS,

II, PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. Third Series. Vol. xvi.
Nos. 94-96. October to December 1865.

H.Seeley.—Ammonites from the Cambridge Greensand, 225 (2 plates).

W. B. Carpenter.—Microscopic Structure of the Shell of Rhyncho-
nella Geiitziana, 305.

FF’. McCoy.—Cretaceous Deposits of Australia, 333.

H. Seeley.—T wo new Plesiosaurs from the Lias, 352 (plate).

J. W. Salter and H. Woodward’s ‘ Chart of Fossil Crustacea,’ noticed,
362,

T. R. Jones and H. B. Holl.—Paleozoic Bivalved Entomostraca.
No. VI. Some Silurian Species (Primitia), 414 (plate).

Leonhard und Geinitz’s Neues Jahrbuch fiir Mineralogie, Geologie,
und Palaontologie. Jahrgang 1865. Hefte 5 & 6.

A. Streng.—Ueber die Zusammensetzung einiger Silicate mit beson-
derer Beriicksichtigung der polymeren Isomorphie, 515.

G. Wurttenberger.—Der Culm und die untere Steinkohlen-Formation
am Kellerwalde in Kurhessen, 5380.

C. Fuchs.—Ueber das specifische Gewicht einiger Silicate, 576.

F. Sandberger.—Ueber Kobalt und Wismuth enthaltende Fahlerze
und deren Oxydations-Produkte, 584.

Letters; Notices of Books, Minerals, Geology, and Fossils.

E. Stohr.—Die Basaltklippe Batu dodol an Javas Ostkuste und ihre
Hebung in der Jetztzeit, 641.

K. v. Fritsch.—Notizen tiber geologische Verhaltnisse im Hegau, 651.

a Se es as den Nephelindolerit von Meiches im Vogelsgebirge,
674.

C. Fuchs und Graebe.—Die Lava der Aetna-Eruption des Jahres
1865, 710.

Letters; Notices of Books, Minerals, Geology, and Fossils.

L’Institut. 1 Section. 33° Année. Nos. 1656-1664.
2° Section. 30° Année. Nos. 357 & 358.
Natural History Review. No. 20. October 1865.

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Ltalies.

Bagot, A. H. Exhibition of 1864. Reply to letter of G. W. Maun-
sell, Esq., of 21st October, 1865. 1865.

Barrande, J. Systéme Silurien du centre de la Bohéme. 1°r¢ Partie.
Recherches Paléontologiques. Vol. u. Céphalopodes. 1* Série.
Planches 14107. 1865.

Brancom, G. G. Studi sul Tarso-Metatarso degli uccelli ed in par-
ticolare su quello dell’ Apyornis maximus.

Bischof, G. Lehrbuch der chemischen und physikalischen Geologie.
Vokai ( AS65)

DONATIONS. —.- 183

Carter, H. J. Description of some of the larger forms of Fossilized
Foraminifera in Sinde, with Observations on their Internal Struc-
ture. 1853. From Sir R. I. Murchison, K.C.B., F.4S8., Se.

- Catullo, T. A. Brocchi, Gio. Battista. 1863.

. Delle Miniere delle Alpi Venete e principalmente di quelle
del Bellunese. 1860.

Discorrimenti sopra alcuni importanti falti geognostico-
paleozoici. 1864.

——. Sopra le Scoperte de chiaro uomo Sig. Dott. Lioy. “1865.

Cocchi, I. Di alcuni Resti Umani e degli oggetti di Umana Indus-
tria dei tempi Preistorici raccolti in Toscana, 1865.

Collenot, J. J La Bréche Osseuse de la montagne de Genay, prés
Semur (Cote-d’Or). 1865.

Deshayes, G. P. Description des animaux sans vertebres découverts
dans le bassin de Paris. Vol. iii. Livr. 4-7. 1865.

Duncan, P.M. <A Description of some Fossil Corals from the South
Australian Tertiaries. 1865. :

Duncan, P. M.,and G. P.Wall. A Notice of the Geology of Jamaica,
especially with reference to the District of Clarendon; with
Descriptions of the Cretaceous, Eocene, and Miocene Corals of the
Island. 1865.

Eck, H. Ueber die Formationen des bunten Sandsteins und des
Muschelkalks in Oberschlesien und ihre Versteinerungen. 1865,

Groot, C. de. Benoeming der Gesteenten aangenomen bij het mijn-
wezen in Nederlandsch-Indie. 1864.

Gutzeit, T. fon. Das Gesez der Zwillingsbildungen am Stein. 1865.

Haast, J. Report on the Geological Exploration of the West Coast
of New Zealand. 1865. |

Report on the Geological Formation of the Timaru District
in reference to obtaining a supply of Water. 1865,

Report on the Headwaters of the River Waitaki. 1865.

Haswell, G. C. On the Silurian Formation of the Pentland Hills.
1865.

Jones, T. R., and H. B. Holl. Notes on the Paleozoic Bivalved
Entomostraca. No. VI. Some Silurian Species (Primitia). 1865.

Leidy, J. Cretaceous Reptiles of the United States. 1865.

Marmora, A.dela. Geologia dell’ isola di Sardegna. (Biographical
Notice by I. Cocchi.) 1857.

Minin. J. Zone a Avicula contorta ou Etage Rheetien. 1865.

184. - : DONATIONS.

Montagna, C. Generazione della Terra metodicamente esposta con
Nuovi Principii di Geologia. Fasce.4&6. From Sir C. Lyell,
Bart. HG Sy Oe. |

Mérch, O. A, L. Catalogus Conchyliorum que reliquit cl. N. Chr.
N. Lassen. 18638.

Mortillet, G. de. Les Terramares du Reggianais, passage des époques
anté-historiques aux temps historiques. 1865.

Ogilvie, G. The Master-Builder’s Plan, or the Principles of Organic ~
Architecture as indicated in the typical forms of animals. 13858.
From Prof. J. Tennant, F.GS., Se.

Omboni, G. Sulle condizioni geologiche delle ferrovie progettate per
arrivare a Covia passando per lo Spluga, il Settimo e il Lucomagno.
1864.

Oppel, A. Die tithonische Etage. 1865.

Parker, W. K., and 7. R&R. Jones. On some Foraminifera from the
North Atlantic and Arctic Oceans, including Davis Straits and
Baffin’s Bay. 1865.

Ponn, G. Il periodo glaciale e Pantichita dell’ uomo. 1865.

Sopra diversi periodi erruttivi determinati nell’ Italia Cen-
trale. Memoria Geologica. 1864.

——. Storia Naturale dell’ agro Pontino. 1865.

Readwin, T, A. Paper on the recent discovery of Gold at Gwyn-
fynydd, Merionethshire. 1865.

Report. Annual Report of the Board of Regents of the Smithsonian
Institution, showing the operations, expenditures, and condition of
the Institution for the year 1863. 1864. From the Snuthsoman

Institution.

——. Report of the Commissioner of Patents for the year 1862.
Arts and Manufactures. 2 vols. 1864. From the Patent Office,
Washington.

Roncont, G. B. Giovanni Arduino et le miniere della Toscana
1865.

Stoliczka, F.. Kine Revision der Gastropoden der Gosauschichten in
den Ostalpen. 1865.

Studer, B. Geologisches aus dem Emmenthal. 1865.
Zur Geologie der Berneralpen.

Suess, H. Ueber Ammoniten. 1865.

Winslow, 0. F. The cooling Globe; or the Mechanics of Geology.
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Woodward, H. Description of a New Chart of Fossil Crustacea, by
J. W. Salter and H. Woodward. 1865,

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

‘THE GEOLOGICAL SOCIETY.

JANUARY 10, 1866.

Woomes Chunder Bonnerjee, Esq., 108 Denbigh Street, St. George’s
Road, S.W.; Charles Pannel, Esq., Torquay; and Joseph Wright,
Esq., 39 Duncan Street, Cork, Ireland, were elected Fellows.

The following communications were read :—

1. On the so-called “ Kozoonat Rocr.” By Professors Witttam Kine
and T. H. Rownzy, of the Queen’s University in Ireland, and the
Queen’s College in Galway*.

[Communicated by Sir Roderick I. Murchison, Bart., K.C.B., &c.}
[Puates XIV. & XV.]

ConTEnNTSs.

~ “Canal-system,”’

. Introduction.
. General description of the che-

mical, mineral, and structural
characters of Grenville ‘‘EKo-
zoonal”’ Ophite.

. General characters of ‘“ Hozoon

Canadense,” including remarks
on Connemara ‘“ EHozoonal’”’

Ophite.

. “Proper wall” of “ Hozoon Ca-

nadense:”’ its variations.
including a

VIL
VILL

IX.

X.
XI.

general description of ‘“ Hozoo-
nal” Ophite from various
places.

. “Stolon-passages.”’

“‘ Sarcode-chambers.”
“Intermediate” or
mentary skeleton.”
Geological evidences bearing on

the nature of “‘ Hozoon Cana-
dense.”
Summary of evidences.
Conclusion.

‘‘ supple-

I. Introduction.

Ovr attention was first directed to the subject of the present memoir
by the communications of Sir William Logan, Dr. Dawson, and

* Since the reading of this paper, it has been revised and augmented, by per-
mission of the Council.
VOL. XXII.—PART I,

P

186 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

Dr. Sterry Hunt, read at the Bath meeting of the British Association,
‘*On the Occurrence of Organic Remains in the Laurentian Rocks of
Canada.” Besides, one of us, when in London last January, ex-
amining specimens of the “‘ remains” in question, and observing how
closely the rock containing them resembled the Ophite* of Conne-
mara, was led to suspect an identity of origin for both deposits.
Our interest in the matter was further excited on reading an
announcement in the ‘ Geological Magazine’ for last February, of the
discovery by Mr. W. A. Sandford, “verified” by Professor T. Rupert
Jones, of ‘ Kozoonal structure in the Connemara marble” 7.

Considering that we resided near the locality which yielded the
latter rock, and that the determination whether, or not, it had resulted
from the growth of “‘ Hozoon Canadense”’ would enable us to form a
positive opinion as to the age of the great metamorphic masses with
which it is interstratified, we felt ourselves called upon to undertake
an investigation promising so important a result.

We commenced with no misgivings as to the “ eozoonal ” origin
of the Canadian Ophite, while our faith in the conclusion come
to by Sir William Logan, and his able coadjutors, was strengthened
by subsequently reading the masterly papers which appeared in
No. 81 of the ‘ Quarterly Journal of the Geological Society.’ Very
few having any knowledge of the construction of the calcareous
encasements of the various foraminifers, whether characterizing the
simple nubecularias or the complex nummulinas, could rise from
the perusal of those papers without feeling more or less disposed to
adopt the view that the Canadian Ophite had originated from the
superpositional, but otherwise indefinite, mode of growth of a gigantic
sessile spreading representative of the lowest known group of animals,
or without admitting that the view was based on sound reasoning
and deep thought.

* The names ophite and serpentine have been indifferently employed by geo-
logists for the rock under description and some others allied to it; but the first
one, which was used by Vitruvius, having priority, we have determined, after
some consideration, on employing it; and as the second is generally applied by
mineralogists to the essential (silicated) mineral of Ophite, we shall restrict it to
this application in the present memoir. By adopting this plan much confusion
will be avoided, especially as many mineralogists and geologists are in the habit
of calling both the rock and its essential mineral by the name of serpentine.
Had it been necessary to call the rock serpentine, the name retinalite (as will be
seen hereafter) might have been retained for the mineral.

Tt Op. cit. vol. 1. p. 88. ;

+ Sir Roderick I. Murchison (Siluria, 2nd edit. p. 192) and Professor Harkness
(Geological Magazine, vol. ii. pp. 147, 148) are of opinion that the Connemara
metamorphic rocks are ‘‘ Lower Silurian.’ From their discordance, both in
strike and dip, with the overlying Upper Silurian beds, their highly altered con-
dition, compared with the latter deposits (both of which circumstances favour
a greater chronogeological gap than is sanctioned by the opinion stated), and
their being devoid of Lower Silurian, Upper Cambrian, or other fossils, one of
us placed them, in an edition of his ‘Synoptical Table of Aqueous Rock-groups,’
in the “Lower Cambrian system—Sedgwick (? Huronian, Logan) ”—thus,
“? Cliffden (Connemara) Quartzites.” This edition was printed in 1862, by
Mr. 8. J. Mackie, F.G.S., editor of the ‘ Geologist,’ and is entitled “Student's
Series, No. 21.”

1866. ] KING AND ROWNEY—“ EOZOONAL ROOK.” 187

II. General Description of the Chemical, Mineral, and Structural
Characters of Grenville “ Hozoonal” Ophite.

In a chemical point of view this. rock consists essentially, Ist, of
hydro-magnesian silicates, the base being often more or less com-
bined with alumina or iron-protoxide ; and, 2nd, of carbonate of lime,
a portion of which is sometimes replaced by carbonate of magnesia.
Mineralogically, it consists of serpentine, pyrosclerite, or loganite,
including their respective varieties, which may be referred to the
first group of substances* ; also calcite and dolomite, which belong to
the second group. These may be regarded as its essential constituent
minerals; but there are occasionally present diopside, pyrallolite,
chondrodite, apatite, mica, pyrites, graphite, giobertite, and others.

Polished specimens of “‘ eozoonal” Ophite, examined by an ordi-
nary magnifier, are seen to consist of a more or less saccharoidal

* Several variously named ophitic minerals are known, which, although differ-
ing structurally, are identical in chemical composition. (a.) Serpentine is amor-
- phous, uneven or conchoidal in fracture, and composed, according to Scheerer’s
analysis of pure specimens from Snarum in Norway, of SiO, 40°74, Mg O 41°48,
HO 12°64, &c. 48:2. Retinalite (Thompson), although stated to contain two or
three per cent. more water, is considered by Sterry Hunt to be the same mineral.
Bowenite, which occurs as scaly aggregations imbedded in saccharoidal calcite,
may be regarded in the same light. (b.) Chrysotile (Kobell), found in layers
often very thin, with a transverse fibrous structure identical with that of ami-
anthus or the finest asbestus, is composed, according to Kobell’s analysis of
specimens from Reichenstein, Silesia (the original locality), of $i O, 43:50,
Mg O 40:00, HO 13:80, &c. 2:48: it passes into picrolite, in which the fibres are
coarse or acicular, adherent laterally, or separated, and not always parallel.
(c.) Metaxite (Breithaupt) occurs in tufts or dendritic aggregations of a dull
or slightly silky lustre, and consists, according to Delesse, whose specimens were
from Reichenstein, of SiO, 42:1, MgO 41:9, HO 136, &. 2-4. Some other
varieties are known, as thermophyllite and marmolite, having a similar chemical
composition. All the foregoing may be regarded as allomorphs of one and the
same mineral species, consisting, if we eliminate the minor ingredients, of
“Silica 43, Magnesia 44, and Water 13” (Delafosse), or 2810,, 3Mg O, 2HO.
There also occur a number of other hydrous silicates of magnesia related to the
one above formulated, agreeing with it in the percentage of HO, but differing
therefrom in containing Al, O,, or Fe, O,, or both, or Ca O,—namely, pyrosclerite,
bastite, loganite, and chonicrite—every one, like serpentine, having its allo-
morphs. Besides, there are allied species containing more or less water, as
deweylite, picrosmine, and others. Confining ourselves to serpentine, pyro-
sclerite, and loganite, these being essentially ophitic, they are respectively re-
presented by an earthy variety—namely, aphrodite, saponite, pseudophite, and
some containing an extra percentage of water. Minerals, it is well known, often
present themselves under various forms without undergoing any chemical change,
and without any relation to the different axial systems in which any one of them
may crystallize. Thus, aragonite occurs (1) compact and amorphous; (2) mas-
sive and cleavable; (3) coralloidal, as flos ferri; (4) asbestiform, as satin spar.
All these varieties are considered to belong to one axial system—the monocli-
nate; but being obviously of other forms than one, and as they are all chemi-
cally alike, we propose to call them allomorphs—from &) os, other, and pop¢y,
form. Calcite is of the same chemical composition as aragonite; the fact, how-
ever, of its belonging to a different axial system—the rhombohedral—makes it a
dimorph, and not, as in the above sense, an allomorph. Like aragonite, calcite
is also subject to allomorphism; and so are a large number of other minerals.
Not being aware that any distinctive term has been applied to the first class of
precited’ modifications, the want of which has often been felt in our present in-
vestigations, we have been induced to propose for it the one already employed.

PB 2

188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

base, and of various-shaped granules, separated, or irregularly united
and clustered together—the latter bemg imbedded in the former.
The base consists of whitish-coloured calcite, or dolomite ; while the
granules, which ‘“‘ vary in size from the tenth to the fourth of an
inch,” are of serpentine, or the allied minerals loganite ‘and pyro- —
sclerite, conspicuous by their green colour of various shades: in some
cases the granules consist of a white crystalline anhydrous mineral
(non-essential in Ophite)—a variety of pyroxene called diopside.
Often the granules are irregularly scattered through the base; and
occasionally a number of them are united so as to form uneyen-
surfaced plates, which affect a more or less parallel arrangement.
Ophite thus presents a spotted or laminated appearance. Besides,
its essential mineral, serpentine, is frequently aggregated into thick
complexly undulating layers, variously intermixed or intercalated
with aggregations of other silicated minerals, chiefly anhydrous, dif-
fering in colour; and the calcite becomes expanded into layers of
saccharoidal marble: under these conditions Ophite assumes features
much more markedly stratified.

Examined with a high power, the granules are seen to be generally
segmented or lobulated. Often the segmentations are very slight ;
and as often they are well pronounced, being here deep narrow
chinks, and there long subcylindrical necks, straight, or tortuous.

The structure and composition of the granules, and their presence
in a calcareous matrix, were first made out in Ophite from Canada,
—nmost satisfactorily in that occurring at Grenville: this variety may
therefore be regarded as typically ‘‘eozoonal,” particularly as the
above characters, and some others less obviously associated with them,
have been considered specially determinative of its “foraminiferal
origin.” This being the case, we propose to include under the name
“ eozoonal” all rocks which do not materially differ in their internal
structure from the one just described.

We have consequently placed in the “eozoonal” section the
varieties of Ophite which occur in Connemara, Donegal, and the
Isle of Skye, as well as others from India, Bavaria, and the State of
Delaware, specimens of all having passed under our examination*.
Ophitic rocks are also found in Anglesea, Saxony, Norway, the
Tyrol, Cornwally, and Switzerland; but in none of them haye we
detected “‘eozoonal” characters,—a circumstanee which, taken in
conjunction with some considerations hereafter noticed, disposes us
to suspect that they belong to a different section.

III. General Characters of ‘‘ Kozoon Canadense,”

According to the view which ascribes the formation of ‘‘ eozoonal”’
Ophite to the growth and reproduction of a foraminifer, the sac-

* We have not had an opportunity of examining any specimens of Ophite
from the Vosges; but from Delesse’s description of this rock (Ann. des Mines,
4e sér, tome xvill. pp. 8309-356), we are led to suspect that some of it will turn
out to be * eozoonal.”

+t From a fact stated hereafter there is some probability that Cornish Ophite
is “‘eozoonal.”’

1866. ] KING AND ROWNEY—“ EOZOONAL ROCK.” 189

charoidal calcite was originally the amorphous calcareous substance
composing the septa which bounded or formed the “ chambers” that
were occupied by its sarcode-segments; while the granules of ser-
pentine are “casts” of the “chambers” themselves. According to
Sterry Hunt, “the vacant spaces left by the decay of the sarcode
may be supposed to have been filled by a process of infiltration, in
which the silicates were deposited from solution in water, like the
silica which fills up the pores of wood in the process of silicification”’*.

Considering the scattered and laminar modes of arrangement of
the “ chamber-casts,” it, is conceived that ‘“‘ Hozoon Canadense”’ be-
came enlarged by the irregular heaping up.or “ acervuline” growth
of the “ sarcode-segments,” as well as by their having grown in suc-
cessive layers one upon another. On this view the calcareous septa,
enclosing the sarcode-segments, formed a vesicular skeleton, its cayi-
ties affecting an “ acervuline,” or a laminar arrangement.

The calcareous septa are in some instances extremely thin, and in
others of considerable thickness. In the latter state they have been
described as consisting of two distinct portions. One of them, con-
sidered to have been the immediate covering of the sarcode sub-
stance, occurs as a thin fibrous or “ asbestiform layer,” the fibres
passing from surface to surface—peculiarities which have given rise
to the idea that the layer was originally the homologue of the finely
tubulated “ proper wall’’ characteristic of the skeleton of Nummu-
lina, Operculina, Calcarina, and other allied foraminiferal genera,
and consequently that the fibres are casts of tubules, such passages
having served for the extrusion of fine thread-like ‘ prolongations,”
called pseudopodia, from the “‘ sarcode-segments :” the other portion,
usually the thickest, and designated, from its position and other con-
siderations, the “‘intermediate skeleton,” contains imbedded in its
substance (this is particularly the case in Canadian Ophite) a variety
of branching and other structures, which are regarded as “internal
casts” of tubular passages, such as are known to constitute the
“canal system” (similarly circumstanced, and occupied by thickish
_ “yprolongations of the sarcode-substance’’) of the foraminifers above
mentioned. Certain of these structures, also some of the elongated
constrictions already noticed, are supposed to be casts of passages
occupied by “stolons,” which connected both vertically adjacent and
laterally adjacent ‘“ sarcode-segments.”

When specimens of ‘“ eozoonal” rock are carefully digested in a
_ weak solution of hydrochloric acid, the calcite may be completely
dissolved out, leaving vacant passages which wind about amidst the
undissolved granules and plates or ‘‘ chamber-casts.” As the branch-
ing structures imbedded in the septa are insoluble in this menstruum,
-like the latter parts they remain intact in the passages. Frequently,
also, the surfaces of the granules may be seen crowded with aciculi
—the so-called casts of the pseudopodial tubuli of the “ proper wall.”

At first our mvestigations were not attended with much success.

* Quart. Journ. Geol. Soc. vol. xxi. p. 67. Dr. Dawson adopts a similar view,
_—that the matter of the chamber-casts was ‘introduced by infiltration or as se-
diment”’ (op. czt. p. 52). Dr. Carpenter, however, holds a different view, which
will be noticed hereafter.

190 | PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Jan. 10,

The Connemara Ophite contained what we had no doubt had been
taken for “‘ chamber-casts ;” but these parts differed in one respect
considerably from those belonging to the Grenville variety. We had
got the impression that in the latter they were rarely arranged other-
wise than in lamine ; but in our home rock we found them to have a
decidedly “‘acervuline” arrangement, and to be seemingly distin-
guished by some other characters.

In this dilemma we made free to apply to Sir William Logan,
ewho very kindly supplied us with specimens from Grenville. These
assisted us materially; for we now saw that the “ acervuline”
arrangement of the “ chamber-casts” was likewise a characteristic
feature of the Canadian Ophite. Still the two rocks presented some
important differences. As we informed Sir William Logan, the
“‘ chamber-casts ” in the variety from our locality varied considerably
in size, some being large, often as much as half an inch in diameter,
and others extremely small; while the septa are often very thin,
resembling in this respect the cell-walls of ordinary vegetable tissue
(parenchyma), and frequently the contrary, in many instances mea-
suring half an inch in thickness. The contrast between the
‘‘ chamber-casts”’ and the septa was not strikingly obvious, owing to
the paleness of the green colour of the former and the greyish
whiteness of the latter. Besides, the septa showed no decided
appearance of being traversed by structures representing the ‘ canal
system.’ We also felt unconvinced of haying detected is Li
examples of the “‘ proper wall”’ or asbestiform layer.

At last, by mere accident, we procured from a dealer in Galway a
specimen, cut in cine darlcta of a bottle, containing ‘ acervuline ”
patches, in which the ‘‘ chamber-casts,” composed of what we con-
sider to be loganite*, and the septa, consisting of white calcite,
were as decidedly in contrast as in Canadian specimens: the agree-
ment was still closer, as the ‘“‘ walls”? were of ordinary thickness, and
they appeared to contain representatives of the “ canal system.”
This proved to be the only specimen we could procure in Galway ;
but learning from the dealer that he recollected where it was got,
we determined on taking him as our guide to the place and trying
to procure more of the same variety.

We had the good fortune to be accompanied in our excursion by
Professor Harkness, who, however, soon showed himself to have no
sympathy with us in the view we then held, being as much a dis-
believer in “ Hozoon Canadense” as Mr. Bailey, who, a few days pre-
viously, had publicly declared his doubts that the “ thing in question
was a fossil at all” 7. Our “ compagnon de voyage” argued for its

* We learn from a paper by Professor Haughton, inserted in the ‘Journal of
the Geological Society of Dublin,’ vol. v. p. 128, that the Rev. Joseph Galbraith
analyzed a specimen of Connemara Ophite, and proved it to be a hydro-mag-
nesian silicate, with a little lime and iron peroxide, from which we infer that it
is impure. Doubtless the rock varies much according to locality: we have
found specimens containing so much alumina as to show their close relationship
.to loganite.

+ Meeting of the Royal Geological Society of Dublin, held April 12th, Mr.
Bailey has since published his view in a note added to his paper on “ The
Cambrian Rocks of the British Islands,” See ‘Geological Magazine,’ vol. ii. p. 388.

1866. ] KING AND ROWNEY—“ EOZOONAL ROCK.” 191

structures being merely the product of crystallization, illustrating
the “ chamber-casts” by a reference to the forms of wavellite, and
referring the “ proper wall” and “canal system” to tremolite*.

We succeeded in making a large collection of specimens at the
principal “ marble-quarries” of Barna-oran, Lisoughter, and Glan-
ochan: the latter place yielded the variety we wanted.

IV. “ Proper wall” of *« Kozoon Canadense.”

Settled quietly before one of Smith and Beck’s first-class binocular
microscopes, and furnished with the best object-glasses and eye-
pieces, we examined a number of specimens, both from Grenville
and Connemara, prepared by polishing and decalcification. While
thus engaged the question occurred to us, If, in the laminar portions
of Ophite, the layers are the result of superpositional growth, how
does it happen that the “ proper wall” of the chambers “ every-
where presents” the tubules which served as passages for the
pseudopods? In this case the wnder as well as the upper side of a
layer of ‘“‘ chambers” must have been tubulated—yjust, in short, as
represented by the transparent section in plate vui. fig. 3a, b,¢,
and in the ideal diagram or woodcut in p. 61, of Dr. Carpenter’s
paper in No. 81 of the ‘ Quarterly Journal of the Geological Society.’
There is no difficulty in conceiving the pseudopods of the exposed
or upper “proper wall” of the top layer of “chambers” to play
their proper part, as they could be freely protruded through and
beyond the orifices of the tubules. But how could those act which
belonged to the wnder “ proper wall,” considering that their egress
would be effectually barred by the upper “proper wall” of the
immediately subjacent layer of ‘“‘chambers”? The difficulty, we
felt persuaded, would be met by the following explanation :—The
two layers were separated by vacant spaces, except at certain points
or places occupied by “‘stolons:” in this case the pseudopods of the
two layers could be freely thrust through the tubules into the
vacancies, where they would be in free communication with the
surrounding medium, and also enabled to elaborate the ‘‘ interme-
diate skeleton.” But, unfortunately for this explanation, it has
been stated that the successive layers of chambers, each having its
own proper wall, are often superposed one upon another without the
intervention of any ‘intermediate skeleton’”’}; also, that “‘ where
there is little trace of the intermediate skeleton between the cham-
bers, the characteristic structure of the proper wall is still unmis-
takeably exhibited ” +.

We next considered that, although it is quite true the “ casts of
the tubules” are often seen standing apart, they also occur so closely
packed together, “‘ standing side by side like the fibres of asbestus,”
as to forbid the idea that there are any interspaces between them.
Again, the tubules must of necessity have had walls. Now if the

* Professor Harkness has stated his opinion before the Geological Section of the
British Association at the Birmingham meeting. See ‘ Reader,’ Sept. 30, 1865.

t Carpenter, Quart. Journ. Geol. Soc. vol. xxi. p. 63, pl. ix. fig. 4.

{ Carpenter, ‘Intellectual Observer,’ vol. vii. p. 294. =

192 , PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

fibres are casts of tubules, how could such be the case in places
where the asbestiform layer, as just noticed, consists of intimately ©
juxtaposed fibres, with nothing between them*? For anything that
we observed to the contrary, the fibres thus circumstanced displayed
quite as little evidence of having been parietally separated as those
of asbestus. Moreover the fibres ‘‘sometimes pass off obliquely or
even tangentially, so as to run for considerable distances in the
chamber-walls,”— a peculiarity which, as it has “no parallel”
among foraminifers, we were disposed to accept as negative evidence
against their foraminiferal origin.

These facts and considerations produced in us in the early stage
of our investigations simply a scepticism as to the organic origin of -
the asbestiform layer. Entertaining no doubt regarding Dawson’s
view of the other structures, we were merely led to gees that this
part was the product of crystallization.

Subsequently our suspicion became a settled conviction on dis- -
covering examples of the “ proper wall” under circumstances which
clearly showed it to be altogether independent of the “calcareous
skeleton.” The conclusion just stated we hold to be demonstrated
by the example represented in fig. 2, Plate XIV., than which nothing
can more intelligibly explain the purely crystalline origin and nature
of the part in question. This remarkably beautiful example, selected
out of a number of the same kind, is taken from an undecalcified
slice of Grenville Ophitet: it consists of three or four closely con-
joined granules of serpentine (a plate of slightly individualized
“‘ chamber-casts ”), having on one side a continuous border of
“proper wall,” which, when examined with a sufficiently high
power, is seen to have, for the most part, a perfectly compact
asbestiform or indefinitely fibrous structure; while in two places
(a and 6) this structure is in an incipient’ ‘state of development,
consisting of a number of parallel thread-like lines clearly and
nee widely separated: the one kind passes into the other.
That it is no other than the serpentine thus crystallized is rendered
evident by the lines in the part marked 6 being extended only
partly across the width of the ‘proper wall,” leaving, without a
shadow of doubt, a narrow external zone of the mineral devoid of all
traces of lineation immediately in contact with, but plainly distinct
from, the “calcareous skeleton.” If, in this case, the “ proper
wall” had been originally calcareous, like the ‘‘ skeleton,” as main-

* In Nummulina levigata we find the width of a parietal interstice between
two adjacent tubules to slightly exceed their diameter; so that casts of the tu-
bules would, if their walls were dissolved out, be separated by strongly-defined
linear openings. Possibly it may be suggested that the ‘appearance of a minute
prismatic arrangement” which nummulines occasionally display, and which is
conceived to have been produced by “ metamorphosis” or “fossilization” (see
Carpenter, Quart. Journ. Geol. Soc. vol. vi. p. 25, and ‘Introduction to the
Study of the Foraminifera,’ p. 270), explains the compact fibrous structure of
the “proper wall” of ‘“‘ Hozoon Canadense ;” but this is obviously too unsatis-
factory a case to be of any assistance, it being merely one of appearance, which
is possibly in some measure due, as believed by Dr. Carpenter, to the “areola-
tion” of the ‘‘tubules,” similar to what prevails in Operculina.

t Our other examples are generally decalcified.

- 1866.] KING AND ROWNEY—“ EOZOONAL ROCK.” 193

tained by Rhizopodists, it never could have presented such appear-
ances; the calcite, and not the serpentine, would have exhibited the
lineated and asbestiform structure. _

Considering that there is an allomorphic variety of serpentine
known as chrysotile, which possesses characters identical with those
of the so-called ‘‘ proper wall,” we feel ourselves warranted in assu-
ming that this part is a layer of the latter mineral.

Moreover, not only does the serpentine become asbestiform, but it
is frequently found changed into a white flocculent substance *, which
takes the place of the “ proper wall ”—oceurring on the surface of
the granules as a crust of varying thickness, and frequently inter-
mixing with the calcite of the skeleton}. Instances have occurred
to us of the serpentine alternately assuming both kinds of structure,
as shown in fig. 3, Plate XIV., which represents a thin transparent
section, seen by transmitted light, of three granules with an irregular
notched border: the projections consist of incipiently chrysotilized
serpentine, and the interspaces or notches of flocculent matter.

The substance under notice has generally a loosish granular tex-
ture ; and often it is compact like starch; it is also rudely lamellar
or prismatic. Occasionally we find it colourless and pellucid, like
chalcedony, and having no appearance of structure under a low
power; but when examined with an object-glass magnifying 350
diameters, it is seen to be fibrous. In short, one of our specimens
of Ophite from Lisoughter shows the surface of a granule of serpen-
tine imperceptibly passing into the asbestiform layer, and this part,
here and there, gradually changing into the flocculent erust; while |
closely adjacent there occurs a mass of the flocculent substance en-
closing, or rather passing wmperceptibly into, asbestiform erystalliza-
tion, the erystals being fine, long, and well developed. 5

The granules are not always furnished with an asbestiform layer,
or a flocculent crust; for highly polished, and consequently trans-
lucent specimens, which have not been submitted to decalcification,
occasionally show them wholly devoid of any covering, their surface
being in immediate contact with the “calcareous skeleton ;”? and in
decaleified specimens we have also seen granules with surfaces quite
smooth, and appearing as if nothing had ever been attached to them.

Reverting to the cases which show the fibres or aciculi of the
asbestiform layer standing apart, attention may be first directed to

* For the sake of brevity and distinction, we propose to name this substance

flocculite—not, however, under the idea of its being a new mineral. Ht is our
present impression that flocculite is merely an allomorph of serpentine; we are
quite ready, nevertheless, to accept it as a chemically different, though closely
related substance. Saponite, pseudophite, and some other allied minerals, are
similarly structureless. Aphrodite, except that its silica and magnesia are in
different relative proportions to those prevailing in serpentine, appears to come
nearest to flocculite. The granalar mineral occurring as a bed in the crystalline
limestone at Grenville, and which Dr. Sterry Hunt has identified with pyrallo-
lite (Geology of Canada, 1863; p. 470), may be identical with it.
’ + In thin transparent sections, examined. by transmitted light, the serpentine
has a metallic appearance resembling brass. Very minute particles of wnchanged
serpentine may be detected by this character, intermixed with the flocculent sub-
stance, both being interspersed amongst the éalcite of the skeleton.

194 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

the one represented in fig. 1, Plate XIV. In this instance there are
two layers belonging to a single granule. The innermost layer is
for the most part perfectly compact and indefinitely fibrous; and,
although not demonstrable, it cannot be considered other than a
modified form of the pertaining serpentine: the outer layer consists
of distinctly individualized fibres or aciculi, generally thick, occa-
sionally very fine, and separated from one another on the left half
(that is, of the figure), but closely adherent by their sides on the
right half, except at their points. The innermost layer is in one place
separately acicular, like the outermost one, showing clearly the
entimate relationship between the two extremes of structure assumed
by the “ proper wall’’*. |

Now such cases as this have been represented as “ exactly cor-
responding” with the fine tubulation characteristic of the shells of
nummuline foraminifers; but from what has already been adduced,
and other evidences to be brought forward, we, on the contrary,
contend for their being merely simulations of such tubulation.

But this case is not to be compared with others we are acquainted
with. We have seen in Grenville Ophite some truly striking examples,
which show the aciculi of the “‘ proper wall” far surpassing in their
mimicry of nummuline tubulation anything hitherto published—
cylindrical rods, uniform in length, thickness, and in their distance
from one another, and standing perpendicularly to the surface of the
‘‘chamber-casts.” At first sight these instances, if studied by them-
selves, might be taken for “internal casts” of tubules; but such a
view speedily vanishes when they are properly examined and studied
in all their relations. Besides being perpendicular, the rods are
occasionally seen leaning, arching, creeping, and twisting about in
all directions: they also unite wholly or partially, converging,
diverging, branching, and anastomosing, so as to produce conical,
cuneiform, dendritic, “‘ brush-like,” and an infinite variety of “bundles,
of which no two are precisely similar.’’ Other aggregations occur,
forming small or wide-spreading patches, which have uniform, or
variously disrupted, surfaces.

Whether viewed transversely or longitudinally, all these modifi-
cations are structurally alike. If examined with a magnifying
power of 350, the patches are seen to consist of ‘closely packed”
parallel fibres—in other words, to have a ‘‘ uniform surface so close
in texture as to be with difficulty resolvable into the points of their
constituent aciculi”+. Place the bundles under the same object-

* This is a case inexplicable on the idea that it has resulted from pseudopo-
dial tubulation; but there is no difficulty in conceiving it to be one of double
allomorphism. The outer layer, which we assume to have been formed first,
has lost its finely fibrous structure, the fibres having become individualized or
transformed into aciculi,—a change characteristic of chrysotile. As the “proper
wall” of Nummulites is formed of a number of laminz, it may be thought that
this double layer is a parallel case; but the tubules, belonging to the former part,
pass uninterruptedly or continuously through the laminz ; whereas in the latter
each of the two layers is composed of an independent series of fibres, or aciculi,

+ It is quite evident Dr. Carpenter has observed examples similar to ours.
See ‘Intellectual Observer,’ vol. vii. p. 292, &e.

1866. ] KING AND ROWNEY—“ EOZOONAL ROCK.” 195

glass, they, too, are seen to have a precisely identical structure,
“every individual thread glistening brightly under appropriate illu-
mination.” Apply the same high power to the rods, even the finest ;
they are likewise resolved into asbestiform fibre*. Does anything
of the kind exist in recent or fossil foraminifers, even in Operculina,
the genus which, owing to its tubuli “ separating from each other in
some parts and becoming more closely crowded in others,” has been
referred to as offering in this respect a complete agreement with
«Kozoon”? Is it conceivable that casts of pseudopodial tubuli
could be compound or fibrous, like asbestus? It is manifestly
superfluous to make a reply in the negative. '

Dr. Carpenter has given representations of the proper wall of
Amphistegina, Operculina, Cycloclypeus, and some other genera;
showing pseudopodial tubulationy; but in every case the tubules
are distinctly separated one from another from base to apex. In
marked contrast to such separation are those cases in ‘‘ eozoonal ”
Ophite, already noticed, in which the casts are intimately united
throughout their entire length.

According to the view we are opposing, the surface of a ‘‘ chamber-
cast’ or granule, from which the “ proper wall” has been detached,
ought to be “rendered hispid by the minute projections which
passed into the entrances of the tubuli,” as in the recent siliceous
casts of an Amphistegina from the Australian coast, described by
Dr. Carpenter; but instead of exhibiting any definite projections,
such as would result from the cylindrical and separated tubula-
tion of the “ proper wall,” like those represented in a “small por-
tion” from another specimen of apparently the same species (‘“‘ to
show the free openings of the tubuli on the internal surface of
the chambers”), the representative part or surface of the serpen-
tine granules, from which the asbestiform layer, whether compact
or open, has been artificially broken off, is irregularly, compactly, and
indefinitely hispid, precisely as obtains on the freshly fractured ter-
minal surfaces of finely fibrous minerals.

It may be contended that the isolated aciculi “ exactly correspond”
with the hispid projections on the siliceous cast of the Amphistegina
just alluded to. This cannot be admitted, since it is impossible to
separate such aciculi from others immediately adjacent, which com-

* Often the asbestiform structure of the aciculi has disappeared, which we
believe to be simply a molecular change. Delesse states that the fibres of chry-
sotile occurring in the Ophite of the Vosges, which are described as “excessively
fine,” ‘“‘swell out and become opaque and whitish on exposure to air” (Ann. des
Mines, 4° sér. tome xviii. p. 328). Taking this fact in connexion with the con-
sideration that Ophite must have passed through considerable variations of tem-
perature, pressure, &c., and that its essential mineral—serpentine—is eminently
unstable in its molecular constitution, as shown by its various allomorphs, we
feel persuaded that our belief, expressed above, cannot be set aside. The modi-
fications presented by the double asbestiform layer, noticed in a previous paper,
and several others which have fallen under our observation, offer an analogy to
the one observed by Delesse.

t Introduction to the Study of the Foraminifera, pl. 13. fig. 25a; pl. 17.
figs. 8, 9,12, 13; pl. 19. figs. 3, 4.

t Op. cit. p. 245, pl. 13. fig. 25 a, and Explanation.

196 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

pletely adhere to one another by their sides: besides, the latter im-
perceptibly pass into the state of an indefinitely fibrous layer. The
examples, and they are numerous, to which reference is made, clearly
show that these modifications belong to one form of crystallization,
and cannot be the result of “ nummuline tubulation.”’ But in order
to place our conclusion beyond the shadow of a doubt, we shall add
another demonstrative evidence to the number already adduced.

We have repeatedly seen fissures in the serpentine—true cracks
striking right across a number of “ chamber-casts” and the inter-
vening calcareous skeleton—filled with calcite and flocculent matter,
separated and intermixed. The conditions of these examples incon-
testably prove that the latter substance is a modification of the
serpentine, and the former an infiltration. One of our specimens
from Lisoughter, which is decaleified, shows the phenomenon most
instructively ; a portion of the flocculent matter still remains, and
the calcite has disappeared. But this is not all: considerable portions
of the walls of the fissure are crowded with as fine examples of
isolated perpendicular parallel aciculi and rods (the latter consisting
‘of asbestiform fibre) as those composing the so-called “ proper wall”
of the adjacent ‘‘chamber-casts”*! Itis unnecessary to add another
sentence by way of evidence or argument in opposition to the view
which ascribes the asbestiform layer to pseudopodial tubulation 7.

Eyidenees strongly in favour of the conclusion that the “ chamber-
casts’? and “ proper wall” were never otherwise than composed of
one and the same mineral substance, have occurred to us in Ophite
from Donegal and from the State of Delaware; the granules of
serpentine, in the former of a dark-green colour, and in the latter
quite yellow, may be observed passing imperceptibly and completely
into the asbestiform condition. We also find exactly the same change
in Ophite (from Snarum in Norway) wholly devoid of anything like
organic structure: a specimen now before us shows here and there
its essential mineral, serpentine, becoming changed into films struc-
turally indistinguishable from the asbestiform covering of *‘ eozoonal ”
sarcode-chambers, even often presenting its identical intermitted and
incipient erystallization. More cogent evidence could not be adduced
to prove that the “‘ proper wall” is no other than an allomorphic
phenomenon.

A strictly identical case, however, and one which may be regarded
as conclusively proving the original mineral nature of the “ proper
wall,” has occurred to us in another mineral. Chondrodite, a spe-

* See Plate XIV. fig. 4, magnified 110 diameters. In this particular example
the aciculi on one of the walls of the fissure are exceedingly minute, being with
difficulty detected except under a power of 210; similar aciculi are interspersed
amongst the larger kind on the opposite wall. The large aciculi at one part of
the wall are closely crowded together: from this condition they graduate into
a compact layer indefinitely fibrous.

+ M. Delesse mentions a fact which equally shows the fallacy of the view
taken by Rhizopodists as to the origin of the asbestiform layer. The Ophite of
Xettes, in the Vosges, contains nodules (les rognons) possessing the mineralogical
characters of granite, surrounded by an envelope composed of radiately fibrous
chrysotile (see Ann. des Mines, 4° sér. tome xvili. p. 339),

“1866. | KING AND KROWNEY—“ EOZOONAL ROCK.”’ 197

cies agreeing with serpentine in its mode of aggregation, is often
found in a finely granular condition imbedded in saccharoidal calcite.
In numerous instances we have found imbedded grains of this mineral
from New Jersey more or less incrusted with an asbestiform layer
which exhibits modifications, speaking advisedly, the exact parallel
of those common to the “ proper wall of Hozoon Canadense.” Three
cases have been selected to illustrate the layer in question. In one of
them, represented in Plate XIV. fig. 5, magnified 120 diameters, the
fibres form a finely asbestiform plate, perfectly compact in texture
except where it curves, lying between two grains of chondrodite,
which plate, when examined with a power of 210, presents exactly
the appearance of translucent compactly fibrous selenite; in the
second case, Pl, XIV. fig. 6, magnified 60 diameters, the fibres are
white, silky, somewhat coarse, rarely otherwise than parallel to one
another, oftenslightly apart, and lying obliquely between two grains ;
in the third, shown in Pl. XIV. fig. 7, magnified 120 diameters, the
fibres are aggregated into very slender, pointed, separated rods, pro-
jecting from one end of a grain. In the last case the interspaces
appear to have been once filled with fibres that have become detached,
possibly by decalcification ; in the others they appear to be the re-
sult of some slight tensional or torsional movements.

Is any naturalist prepared to assent to the notion that in these
examples the asbestiform layer represents the “ proper wall” of a
foraminifer, and that the fibres are casts of pseudopodial tubules ?
If not, he must at once relinquish his belief in the “ nummuline
tubulation ”’ diagnosed, for the investment of the granules of serpen-
tine, as characteristic of “ eozoonal”’ Ophite.

Before concluding the present section, it is necessary to give a
general description of the coat belonging to the serpentine of Con-
nemara Ophite. Like that characterizing the granules of the Gren-
ville rock, the coat is both fibrous and flocculent, both modifications
being often intermixed, distinctly separated or changing imperceptibly
into ‘each other; but in the former state, instead of being generally
composed of parallel fibres, it consists of acicular crystals radiately
or divergently disposed, or variously intersecting one another, also
occasionally curving or twisting, forming aggregations or tufts irre-
gularly dispersed over the granules. Occasionally, however, as in
the cases already noticed, the granules are covered with a true
asbestiform layer, its fibres standing perpendicularly, parallel to one
another, and completely adhering by their sides or separated—offer-
ing in every respect the most perfect agreement with the corre-
sponding part in Grenville ‘‘eozoonal” Ophite*. The flocculent
coat closely resembles that which has been described as character-
istie of the latter rock: it varies from a mere film to a covering of
considerable thickness, a granule often having half of its mass floc-
culent and its other half composed of translucent serpentine, both
varieties being clearly modifications of each other. An example
from Lisoughter, magnified 210 diameters, is represented in fig. 9,

* In addition ;to;the specimens from Lisoughter, at which place we collected

by far the finest examples exhibiting the “proper wall,” we have detected this
part in Ophite from Barna-oran and Glanochan,

198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

Plate XIV., which shows the layer flocculent here and fibrous there :
in the latter state the constituent aciculi are generally parallel, and
in one place divergent*. Such examples clearly form independent
and decisive testimony in favour of the conclusion we have come
to with respect to the corresponding structural modifications pre-
sented by the granules of serpentine in Grenville Ophite—that they
are allomorphic conditions of one and the same substancey.

With respect to the cases of isolated rods, and other modifications of the
asbestiform layer, Dr. Carpenter has incidently mentioned that this part “is
often thrown off by the disengagement of gas in the process of decalcification” f.
Instances of the kind have occurred to us in the specimen presenting the double
layer: loose fibres are seen hanging on the free side of the outer one; and the
innermost is for a considerable extent separated from the surface of the granule.
We have also seen portions of the flocculent coat lying loose in the decalcified
passages, and others raised above the plane of the section. At one time we ©
were disposed to believe that decalcification, likewise internal movements which
the rock has evidently undergone, as well as mechanical action consequent on
breaking, grinding down, and otherwise preparing specimens for examination,
had mainly contributed to produce the cases under notice ; but we are now more
inclined to consider them for the most part to be the result of other agencies.

It has been made clear that Serpentine is transformed into both the asbesti-
form layer and the flocculent coat, and that the former of these epigenes is
converted into the latter. Was the process elaborated solely during some
remote “primordial” period? Had the Grenville Ophite precisely the same
structure it now possesses previously to the deposition of the rocks transgressive
to it§? Has it remained chemically and structurally unaltered during the
immensity of time which has intervened between the Potsdam (Cambrian)
period and the present epoch? We are certainly strongly indisposed to answer
in the affirmative to these questions. For why may not pseudomorphice, allo-
morphic, and other metamorphosing actions, induced by heat, pressure, elec-
tricity, gaseous and hydrous permeations, have been going on throughout all
such time, more or less changing the Serpentine into flocculent matter, trans-
ferring the latter from the granules, and replacing it by their imbedding calcite,
or intermixing it with the latter body, or variously substituting the chemical
constituents of the Serpentine by their isomorphous compounds? These re-
marks express our hypothesis as to the changes which have been and are being
effected in the essential minerals of: ‘‘ Hozoonal” Ophite, and we believe that it

* So many instances have occurred to us, showing the changes mentioned in
the text, that we could readily fill a Plate with them. We could have shown
much finer examples of the asbestiform layer; but the one selected for illustra-
tion has been given because it shows, what is rare, the parallel and divergent
aciculi associated on one granule.

+ Professor Tennant has kindly presented us with a beautiful “moss agate”
of transparent chalcedony, enclosing a number of vermicular bodies, variously
knotted, which appear to be composed of yellowish ferruginous matter; in
some cases they are completely invested with a dense crop of subparallel acicular
crystals, seemingly of the same substance, which penetrate the chalcedony, and
form a well-defined coat remarkably uniform in thickness (see fig. 16, Plate XV.).
This case is a proof that certain substances shoot out from the surface of the
‘body they form, as crystals, and, as such, penetrate a dissimilar surrounding
medium, in a fluid, gelatinous, earthy, or otherwise yielding condition. A similar
origin might with some reason be advanced to account for the aciculi on the
granules of Serpentine; but we regard the conclusion already adopted as too
clearly established to be induced to entertain any other.

+ Intellectual Observer, vol. vii. p. 292.

§ We allude to the Potsdam sandstone, beds of which occur, both in Canada
and in the northern parts of the State of New York, unconformably overlying
highly contorted Laurentian rocks, and composed in many places of pebbles of
the latter in their metamorphosed condition (see Geology of Canada, p. 96).

1866. | KING AND ROWNEY—‘“ EOZOONAL ROCK.” . 199

is sustained by many of the pseudomorphic phenomena made known of late
years by Bischof, Breithaupt, Blum, Daubrée, Delesse, Fallou, Fournet, Muller,
G. Rose, and others.

We offer this hypothesis to explain the intermixture of flocculent matter and
calcite, which occurs so commonly in the so-called skeleton of ‘‘ Hozoon,” and
the change of the surfaces of its ‘‘ chamber-casts” into chrysotile and flocculent
matter; also to account for the occasional absence of the latter two substances
from the surfaces of the ‘‘ chamber-casts,” and their replacement by calcite: in
short, we offer it in explanation of most of the cases of isolated actewli, rods,
bundles, and patches of the asbestiform layer and the fillings in of their separating
spaces by calcite.

V. “ Canal-System” of “ Kozoon Canadense.”

_ Although feeling it necessary to relinquish the idea of the “‘ asbes-
tiform layer” having been originally an organic structure, we still
adhered for some time afterwards to the foraminiferal origin of
Ophite. But having made, as we conceived, an important recti-
fication in the diagnosis of “ Hozoon Canadense,” we naturally felt
ourselves stimulated to endeavour to elucidate the “ canal-system,”
which it was considered had in certain instances been confounded
with “ stolon-passages.” |
It is unnecessary for us to give a history of our investigations
into the speciality now entered upon; suffice it to say that the
longer we examined the more our opinions became unsettled.
Something new was continually turning up to the prejudice of the
belief we had firmly and tenaciously adhered to; so that at last we
found ourselves under the necessity of completely abandoning a point
which had often proved a sheet-anchor whenever either of us was
losing ground in our mutual discussions*.
Lying in the decalcified passages of both Canadian and other
varieties of “‘ eozoonal” Ophite, of the Connemara variety especially,
there are frequently seen irregularly shaped ‘amorphous masses ”
of a mineral substance slightly compact in texture, of a milk-white
colour, and lustreless like starch. Neither Dawson nor Sterry Hunt
has alluded to them ; and Carpenter, by whom they appear to have
been overlooked at first, has only briefly described the Canadian
examples in his last paper, published in the ‘ Intellectual Observer.’
He finds them “to consist in some instances of parallel lamella,
disposed like the leaves of a book, and in others of solid bunches of
rounded filaments, reminding one of a sailor’s ‘swab.’” The Cana-
dian examples are apparently more compact in texture than the
Irish. When detached and crushed, a quarter-inch object-glass
discloses in the former a more or less granular, and in the latter a
somewhat fibrous structure.
Besides the foregoing, there are present, especially in Grenville
Ophite, the simple and branching structures noticed in the early
part of this memoir, or, as they have been named, “ definite shapes,”

* As soon as we had become fully convinced that all the parts of “ Hozoon
Canadense” were of mineral or crystalline origin, we announced the circum-
stance in one of the weekly periodicals, promising at the same time to lay before
the public at an early opportunity the various evidences and considerations
which sustained us in our views, (See ‘Reader,’ June 10, 1865, p. 660.)

— 200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

which “ differ remarkably in size and form,” being caulescent, scopi-
form, ramose, dendritic, claviform, or sheaf-like, and resembling in
many respects certain cryptocrystalline aggregations known to mi-
neralogists. They occur in immediate contact with the “‘ chamber-
casts,” rising directly out of them, occasionally resting against the
asbestiform layer, likewise seemingly in no way connected with
anything, being in appearance isolately imbedded in the calcite of
the septa*. In general their physical characters have a resemblance
to those of the ‘‘ white amorphous masses,’ excepting that they are
somewhat more compact, and have a lustre and colour, especially in
their centre, approaching to the translucency and green tint of the
“‘ chamber-casts.”

Comparing the “amorphous masses” with the “definite shapes,”
there is certainly considerable dissimilarity between them; never-
theless the more examples we examined, the more we felt ourselves
constrained to agree with Dr. Carpenter that both are modifications
of one typet. But as regards their origin, we are under the necessity
of entirely discarding the opinion which ascribes it to organic
structures. /

Previously, however, to going into this question, we deem it right
to show that similar bodies, more or less agreeing with the “ amor-
phous masses ”’ and “ definite shapes,” are not uncommon as imbedded
crystalline aggregations. The subject hitherto has received but little
attention, all that is known of it being confined to a few papers
which seem to have attracted scarcely any notice.

As far back as 1813 and 1815, Dr. Macculloch brought under the
notice of the Geological Society some singular. vermicular ‘forms
in which chlorite is disposed,” occurring in chalcedony and quartz¢ ;
and in 1849, Francis Alger briefly described some similar “‘ imitative
shapes”’ of mica enclosed in crystals of quartz from Vermont, which,
had they occurred in “‘eozoonal rock,” would have been taken for
casts of tortuous canals$. Native metals, notably copper and silver,
likewise metallic oxides, are well known to occur as imbedded arbo-
rescences||. The Museum of Trinity College, Dublin, contains a
beautiful arborescent example of native silver, imbedded in calcite,
strikingly resembling the dendritic ramifications in Grenville Ophite ;
and there is now before us a singularly apposite specimen, of a less
complex character however, for which we are indebted to Dr. Frazer
of Dublin, consisting of slender simple as well as branching stems
of pyrites, imbedded in the same kind of matrix. But it is from
decalcification that the most important results may be expected to
be obtained in our favour. Many of the examples of the so-called
‘siliceous skeleton,’ got by M. Alphonse Gages from various rock-

* In polished specimens of Grenville Ophite, both the “ amorphous masses”
and the “definite shapes” may with a good pocket-lens often be detected lying
imbedded in the calcite of the septa, from which they are well distinguished by
their milk-white appearance.

+ See ‘Intellectual Observer,’ vol. vii. pp. 293, 294.

+ Trans. Geol. Soc. Ist ser. vol. ii. pl. 36. figs. 2&3; also vol. iv. pl. 27. fig. 1.

§ American Journal of Science, 2nd ser. vol. x. pp. 14.& 15.

|| Most specimens of the kind seen in cabinets are partially or wholly decalcified.

—1866.] KING AND ROWNEY—“ EOZOONAL ROCK.” 201

Specimens which he digested, are, in our opinion, homologous to the
“definite shapes” *. Pieces of impure “primary” marble from
Barna-Oran, Connemara, treated in the same way, have yielded to
us numerous aggregations of crystals apparently belonging to actino-
lite. Another marble of the like kind, from a neighbouring locality,
contains irregular lumps, having a lamello-prismatic structure, which
appear to be diopside. A very impure “ primary ” limestone, from
Donegal, containing large crystals of a brown mineral, apparently
Epidote, is filled with prismatic masses, the prisms being either
parallel or radiating. These examples have certainly no resemblance
to the “definite shapes ;’’ but it will shortly be seen that there is a
relationship between the former and certain representatives of the
latter occurring in different varieties of ‘ eozoonal” Ophite.

The so-called “ Moss-agates ” often contain beautiful arborescent
and foliated forms. The specimen already noticed contains a number
of thickish vermicular shapes, seemingly composed of hydrous per-
oxide of iron: their branchings and anastomosings, amidst a mass
of transparent chalcedony, forcibly remind one of some of the simplest
of the “definite shapes.’ We have also in our possession a beautiful
specimen, obtained along with a large number collected at Oberstein,
which is crowded with slender cylindrical dendritic ramifications,
red, green, and yellow, evidently all hydrous oxides of iron: several
of these so decidedly resemble the more complex structures in ques-
tion as to surprise us that no one has suggested the possibility of
their identity of origin. For our part, we unhesitatingly accept
this last case as proving that the so-called “canal-system” of
*« Hozoon Canadense” is a phenomenon of “ imitative crystallization.”

Perhaps none of the imbedded crystallizations we have brought
forward agree chemically with the “ definite shapes.” Those which
are most nearly allied to them in this respect do not present their
identical form. ‘There is a case, however, as yet unnoticed, against
which such an objection cannot be urged—namely, metaxite from
Reichenstein. This mineral, which occurs imbedded in saccharoidal
calcite, crystallizes in ramose and dendritic forms of a pale-green or
whitish colour, opaque or somewhat porcellanous, and compact
or fibro-foliaceous in texture. The crystallizations occur both erect
and spreading: our largest specimen is about an inch in diameter ;
but they are found much less. One of our smallest, obtained by de-
calcification, is represented in Pl. XV. fig. 12, magnified110 diameters.
It is undistinguishable from some of the palmated dendritic “ definite
shapes ” characteristic of Grenville and Connemara Opbite; and, ac-
cording to Delesse’s analysis, it is doubtless chemically identical with
themt. We have therefore no hesitation in concluding that the so-
called “‘ representatives of the canal-system ” of “ Hozoon Canadense”’
are no other than crystallizations of metaxite, an allomorphic variety
of serpentine. |

Reverting to the “amorphous masses,’ Dr. Carpenter, while
investigating the structure of “ eozoonal”’ Ophite, undoubtedly passed

* See ‘Philosophical Magazine,’ 4th ser. vol. xvii. pp. 169-176.
t See analysis of metaxite in a preceding page.
VOL, XXII,—PART I, . o

202 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 10,

beyond the lines reached by others. He made discoveries which,
followed to their legitimate issue, clearly show that the explanation
advanced by Dawson and Sterry Hunt as to the filling in of the
“‘chambers” and other presumed sarcode-encasements is at fault.

The “amorphous masses,” as will be seen by referring to fig. 17,
Pl. XYV., occasionally assume a prismatic structure, with the prisms
closely adherent to one another laterally. We presume that this
example, if not strictly identical with, is closely related to those
which have been described as consisting of “parallel lamelle dis-
posed like the leaves of a book,” or of solid bunches of rounded fila-
ments, reminding one of a sailor’s ‘swab.’” The “nature” of these
bodies “was for a long time a puzzle” to Dr. Carpenter; but,
doubtless perceiving that they are often compact and solid—that their
“parallel lamellze ” and “rounded filaments” have not been bounded
by walls, the conclusion is drawn that they are “are in each case
but a mere aggregation of the elementary forms of sarcode-prolonga-
tion:” in what way will be seen immediately. Thus the same diffi-
culty or puzzle meets us here which we encountered when consider-
ing the nature of the asbestiform layer, numerous examples of which,
it will be recollected, showed no appearance of its presumed pseudo-
podial tubules having been separated by parietal partitions.

Now, considering that, on the foraminiferal view, all the parts of
“* Hozoon Canadense,’’ with the exception of the “ intermediate skele-
ton,” must be regarded as the result of infiltration, mechanical or
chemical, it is obvious that the mode in which this process has been
effected is of primary importance in the main question under discus-
sion; we may therefore be excused accepting any explanation of the
process, unless it accounts for the present appearances of all the
presumed sarcode-encasements.

Dr. Dawson and Dr. Sterry Hunt’s explanation, although simple,
scientific, and supported by numerous cases among existing and
fossil foraminifers, becomes’a failure if carried beyond the “ chamber-
casts” and the ramose or branching representative of the “canal-
system.” Dr. Carpenter has proposed another, which, although in-
tended toaccount for the usual appearances of the “amorphous masses”
and the “asbestiform layer,’ has failed in our opimion more
signally—no known fact or principle of geology, mineralogy, pale-
ontology, and chemistry being known, as far as we are cognizant of
them, to support the view that “the siliceous mineral found its way
into the cavities of the Kozoon, not by mere mechanical m/filtration
occasioned by pressure from without, but by a process of chemical
substitution, which took place, particle by particle, between the sarcode-
body of the animal and certain constituents of the ocean waters,
before the destruction of the former by ordinary decomposition” *.

* The italics are Dr. Carpenter’s. This hypothesis is more fully given in
the Intellectual Observer, vol. vii. p. 290, and p. 294 (upper paragraph); also
in the Proceedings of the Royal Society of London, vol. xiii. p. 546. Having
never seen any account of the suggestion made by Professor Milne-Edwards
‘with regard to the infiltration of fossil bones and teeth, in the course of the
discussion which took place on the Abbeville jaw,” we are necessarily unac-

1866.] KING AND ROWNEY—* EOZOONAL ROCK,” 203

We feel ourselves next called upon to show that the “ amorphous
masses ” are purely of mineral or inorganic origin.

The Canadian examples of these bodies are remarkably uniform in
possessing no more than a rude divisional structure and a starch-
like dullness; but occasionally they present a different appearance.
Referring again to figure 17, the specimen which it represents has a
somewhat rhomboidal shape, a well-defined prismatic structure, and
an incipient lustre: its prisms are for the most part parallel and
closely adherent to one another; but at the sides they separate,
diverge, or curve outwardly, thus approximating to the scopiform
and sheaf=like “ definite shapes” *.

In these compact specimens the divisional structure is so essentially
mineral, such as may be seen in tremolite, kyanite, wollastonite,
scapolite, d&c., as to prevent any mineralogist believing otherwise
than that it is in no respect related to anything organic: and the
belief is powerfully supported by the fact that specimens approxi-
mately similar, both in form and structure, are common, as men-
tioned before, imbedded in some of the primary calcareous marbles
of Connemara and Donegal ; nay, it may be regarded as demonstrated
by the occurrence of similar prismatic specimens which we find lying
adjacent to grains of chondrodite in saccharoidal calcite.
~ The “ definite shapes” are essentially Canadian, since rarely are
they detected in Ophite from other places. For along time our de-
calcifications of Connemara specimens of this rock yielded no more
than a few imperfectly formed rod-like and caulescent bodies, which
differ mainly from the simplest of the Canadian forms in having a
more crystalline appearance. We have been rewarded, however,
just before finishing this paper, by the discovery in Ophite from
Glanochan and Lisoughter of perfectly genuine examples—complex
ramose and dendritic forms, with more or less cylindrical stems and
branches—which occur crowding the decalcified passages. Both in
appearance, and circumstances of occurrence, they cannot be ‘dis-
tinguished from ordinary examples in Grenville Ophitet; and they
closely resemble those figured by Dawson+, Carpenter §, and Rupert
Jones ||. 5

Nothing of the kind has yet occurred to us in any varieties of
Ophite we have examined from the Isle of Skye, India, Donegal,

quainted with it; but possibly its bearing has been misunderstood, as certainly
is Dr. Sterry Hunt’s opinion (thus stated by Dr. Carpenter), ‘“ that the siliceous
infiltration of the cavities of the Eozoon was the result of changes occurring
oe decomposition of the animal.” (See Proc. Roy. Soc. London, vol. xiii.
p- 546.

* Another specimen before us approaches still nearer to the sheaf-like forms
by having all the prisms, which are somewhat apart, ranged in two divergent
series.

t Whatever doubts may have hitherto existed in the mind of some as to the
Connemara Ophite being ‘‘eozoonal,” the existence therein of the “definite
shapes” and the “ proper wall” completely identifies it with that from Grenville.

{ Quart. Journ. Geol. Soc. vol. xxi. pl. vii. fig. 4.

§ Lbed. pl. viii. fig. 5 b,c.

| Popular Science Review, vol. iv. pl. xv. figs. 6 and 7. 5

Q

204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

Bavaria, and the State of Delaware. In the Skye variety, the
decalcified passages exhibit, in addition to the “‘ white amorphous
masses,” several thickish dendritic aggregations, composed of minute
granules, which agree in colour, and apparently in composition, with
the “ chamber-casts” *.

The passages in the Indian Ophite contain a few ill-defined
branching bodies of a somewhat crystalline appearance, along with a
large number of six-sided tabular crystals, apparently of chlorite,
which cross the passages in all directions‘.

The Donegal Ophite contains an abundance of crystalline aggre-
gations similarly situated—and, in addition, a number of plates, some
laminated, and others formed of intersecting crystals, which appear
to correspond to the Canadian and Connemara “ amorphous masses”’t.

The Delaware Ophite is somewhat different, inasmuch as the
crystalline aggregations and amorphous masses are oftener closely
associated than usual; and the former are frequently masked with the
latter. The crystals of the aggregations sometimes assume a den-
dritic disposition ; but they are more generally interlacing, and thus
form thickish reticulated plates. A number of associated passages are
occasionally nearly filled with amorphous (7. ¢. flocculent) matter,
broken up into parallel or divergent plates, with a loose texture§.

In a variety of Ophite from Bavaria, a specimen of which has been
obligingly presented to us by Sir Charles Lyell, Bart., the decalcified
passages contain a large number of white crystalline tufts, more or
less resembling those characterizing the Donegal and Connemara
rocks. ‘They are unaccompanied, however, by crystals of mica,

* In the Isle of Skye Ophite, the ‘‘chamber-casts,” which affect a sort of
lamino-acervuline arrangement, have the ordinary form and mode of attach-
ment, and consist of a dull-white or pale-green serpentine, or possibly pyro-
sclerite: they are small, and much crowded together, resembling in these
respects the granules in some of our Lisoughter specimens. The decalcified.
passages, in addition to the ‘‘amorphous masses” and. ‘“‘ dendritic aggregations ”
noticed in the text, are filled with very minute filiform crystals, similar to those
occurring, as will be seen hereafter, under the same circumstances in Grenville
and Connemara Ophite. The “ chamber-casts” are occasionally invested with
the ‘“ proper wall, which consists of both parallel and divergent aciculi. Hence
no doubt can be entertained as to the “‘eozoonal” character of the Isle of Skye
Ophite.

* The ‘‘chamber-casts”’ of this variety are connected as ordinarily, and ar-
ranged acervulinely, but aggregated into various groups, differently coloured,
a group consisting of either green, blue, buff, or white granules of serpentine (?).
In some groups the granules are unusually small. ‘The various colours give a
beautiful appearance to this Ophite.

t The plates occasionally consist internally of serpentine, more or less split
up, and coated with white crystals. Nay, the serpentine of the ‘‘ chamber-casts”
may be seen similarly divided, also changing into a substance resembling that
of the “amorphous masses.”

§ The asbestiform investment, which the “ chamber-casts” or granules of the
Delaware Ophite usually display, has already been noticed. The latter, com-
posed of a yellowish-coloured serpentine (?), are imbedded in saccharoidal
calcite. They are more irregularly shaped and of larger size than usual, often
completely separated and wide apart, frequently attached to one another by
long neck-like connecting pieces, and acervuline in their arrangement. We are
indebted to the Rey. Dr. Haughton for this variety, as well as that from India,

1866. | KING AND ROWNEY—“ EOZOONAL ROCK.” 205

pyrosclerite, chlorite, &c.; but associated with them are numerous
“white amorphous masses” of a granular texture—some vitreous, and
others opaque. The tufts are aggregations of stout, tapering, slightly
translucent crystals, which divide or rudely radiate, strike off from
points on the surface of the ‘“chamber-casts,” spring’ out of the
‘amorphous masses,” or lie imbedded in the residual calcite of the
passages. The crystals are not so slender as those in the Conne-
mara Ophite; nor do any of them, individually or aggregately, show
such a decided tendency as those of the latter rock to simulate the
Canadian dendritic ramifications*.

If so few “ definite shapes” occur in the Connemara Ophite, they
are undoubtedly well represented by numerous crystalline aggrega-
tions, which, together with the “amorphous masses,” occupy the
decalcified passages, often to the almost entire exclusion of the cal-
careous matter proper to the “skeleton” or septat. Tho crystals,
which are avicular, and separated, or in contact, variously diverge,
radiate, or intersect one another, shooting athwart the passages in
all directions. The aggregations may be completely followed into
the true “ definite shapes,” already noticed, through a variety of in-
termediate forms 7.

The conformity between the Connemara and Grenville varieties
of Ophite, declares Dr. Carpenter, “is so close as to leave no doubt
on my mind as to the organic origin of the former.” ‘I find, in place
of a continuous asbestiform layer covering the segments§, long
straight, bundles of asbestiform filaments radiating from them.
What is the import of these—whether they represent a part of the
original structure of the animal, or are (as I am disposed to suspect)
a product of subsequent metamorphism—is a point which must be
reserved for further investigation’’||. If our interpretation of the
supposition contained in this passage be correct, it implies that, in
Dr. Carpenter’s opinion, the crystalline aggregations were originally
“definite shapes” —internal casts of tubular passages—which have

* This Ophite presents a somewhat unusual appearance, inasmuch as the
“chamber-casts” are aggregated in the form of comparatively thin plates,
which frequently anastomose, producing a sort of network, its meshes, which
are wide, being the “calcareous septa.” Nor are the “‘ chamber-casts” in general
so neatly segmented as in other varieties of Ophite. They are composed of two
kinds of minerals: one, of an impure leek-green colour, displays, on fracture,
a lamellar cleavage, with pearly planes ; the other is darker, often quite black.
The former is possibly pyrosclerite, and the latter may be impure loganite.
‘They are occasionally coated with a forest of short slender diverging crystals,
which might be taken to represent the ‘“‘ proper wall.”

t See Pl. XV. fig. 13. In this example the crystalline aggregations are less
numerous than usual, and they are remarkably free from the “ white amorphous
masses. ”

¢t We find these aggregations to be soluble in hot sulphuric acid, like the
. granules and other ‘“‘eozoonal” parts; from which it may be inferred that they
are composed of a hydrous silicated magnesia, and consequently cannot belong
to a variety of pyroxene or augite. They probably represent another allomorph
of serpentine, and are in all probability a more crystalline form of metaxite.

§ The asbestiform layer, however, as will have beon seen, does exist in Con-
nemara Ophite.

|| Intellectual Observer, vol. vii. pp. 297, 298.

206 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

lost their original forms (cylindrical, flattened, or branching) through
superinduced crystallization. If such an hypothesis be admitted,
the imbedded crystalline aggregations, with which many of the Con-
nemara, Donegal, and other saccharoidal marbles are loaded, may be
considered, with equal reason, to be the metamorphosed or crystallized
representatives of the “ canal-system of Hozoon.’’ Another consider-
ation may be adduced: Ophite, consisting of dark-green serpentine,
or more probably loganite, is of common occurrence at Lisoughter,
intermixed with, and passing into white or yellowish crystalline tufts,
averaging an inch in length. We find the latter to be structurally
and, to all appearance, chemically identical with the micro-crystal-
line aggregations which occur in the true ‘‘ eozoonal” variety from
the same place.

Now we would ask any mineralogist to make himself acquainted
with the known modifications of the “ canal-system” of foraminifers*,
and to conceive the possibility of such modifications assuming cha-
racters identical in every respect with ordinary scopiform crystal-
lization—precisely such as are met with among zeolites, kermesite,
and a number of other minerals+. Let him compare the latter with
the presumed metamorphosed representative of the “‘ canal-system,”
given in figure 14, Pl. XV., magnified 210 diameters, of which the
original occurs in a decalcified specimen of “‘ eozoonal’’ Ophite from
Lisoughter ; and let him consider that this is a fair example of what
he is required to believe was once “an internal cast of an arbores-
cent ‘cluster’ of passages originally occupied with sarcodic prolonga-
tions.”

The dissimilarities existing between the “definite shapes” and
the crystalline aggregations are simply such as obtain among a
number of mineralst. Aragonite differentiates itself in a similar
manner, being crystallized or coralloidal according to circumstances§.
Native silver is perhaps more in point, as beautiful dendritic forms,
some composed of microscopic crystals, others of the metal in the
amorphous state, frequently occur imbedded in calcite.

But admitting in the widest sense the dissimilarities which have
been noticed, they nevertheless do not, in our opinion, weaken in the

* Numerous examples are given in Carpenter’s ‘ Introduction to the Study
of the Foraminifera.’

+ Fossil corals, echinoderms, and shells may have their skeletons replaced
by dolomite, calcite, selenite, and other mineral substances; but we confess to_
be unacquainted with a single instance in which a portion of this part has be-
come transformed into crystals passing beyond its surface. As a case in point,
the corals occurring in the dioritic rock of Rothau, in the Vosges, are changed
into hornblende, garnet, and axinite, without any alteration of form. (See
‘ Annales des Mines,’ 5€ série, vol. xii. p. 318.)

¢ To show one of the principal differences referred to, we may instance the
example under fig. 3 in the ‘tinted plate” appended to Dr. Carpenter’s paper
in the ‘ Intellectual Observer, and the one represented in our figure 14, pl. XV.

§ Beudant has given, in his ‘ Minéralogie,’ p. 49, a representation of a coral-
loidal form of Aragonite, which strikingly resembles the “representative of the
canal-system,” given by Dr. Carpenter in the plate cited in the last note. Of.
course the former may have been developed in a fluid medium,—a condition,
however, to which we do not attach much importance,

1866. ] KING AND ROWNEY—“ EOZOONAL ROCK.” 207

least the view we have taken as to the origin of the “definite
shapes ;” rather the contrary, inasmuch as if it be admitted that
these parts represent an essential structural element, like the
“‘canal-system” of certain existing foraminifers, it follows that
what are considered to be the fossilized remains of the system in
Ophite from the other side of the Atlantic ought to be present in
that occurring in other countries, provided the two rocks agree in
other essential respects. Now the “definite shapes” imbedded in
the calcareous “septa” of the Canadian Ophite are relatively situ-
ated just as the crystalline aggregations are in the Irish and other
varieties.

Reviewing all that has been brought forward in connexion with
the subject before us, what other conclusion can we come to than
that it is of crystalline origin*? Lastly, the “very remarkable dif-
ferences in size and form” which the “definite shapes” display is
opposed to the idea of their being representatives of the “ canal-
system,”—considering that Nature generally adheres to uniformity
of plan in essential parts, even amongst the lowest animal organisms,
and, more especially, that no such ‘‘ very remarkable differences”
have been seen to characterize the “ canal-system” of any known
foraminifer, fossil or recent.

VI. “ Stolon-passages.”

No one having examined specimens of the various kinds of
** eozoonal” Ophite can read the papers by Dawson, Carpenter, and
Rupert Jones, without arriving at the conclusion that certain simple
forms, which they have regarded as “ casts of stolon-passages,” are
only modifications of other structures associated with them. We
possess some remarkably fine specimens of the rock from Lisoughter,
in which may be frequently seen, not only a long scopiform tuft,
composed of divergent or subparallel crystals, forming a union
between two “ chamber-casts ” or granules of serpentine, but occa-
sionally a well-defined plate holding the same office: in some in-
stances as many as three separated parallel plates are seen lying
together. The latter have frequently a granular texture, like that
of the “‘ white amorphous masses;” occasionally, however, they
are somewhat compact, slightly translucent, and of a greenish-white
colour. Thus, “stolon-passages” are formed by representatives both
of the “ definite shapes,’ and the “ chamber-casts.” Fig. 13, Pl. XV.
shows a decalcified specimen from Lisoughter, magnified 25 diameters
times, containing a well-marked case of three adjacent granules united
by means of crystalline tufts ; also another (in the middle of the lower
part of the figure), consisting of two granules connected by three
slightly granular plates: this last is additionally illustrated in fig. 15,
Pl. XV., magnified 120 diameters. One of these granules is con-

* Canadian “eozoonal” rock, it would appear, does not always differ, in its
“representatives of the canal-system,” from Connemara Ophite, inasmuch as
Dr. Dawson notices specimens in which there is a “development of certain
dendritic crystallizations.” Are these in place of the “definite shapes”? (See
Quart. Journ. Geol. Soe, yol. xxi. p. 68.)

208 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan, 10,

nected with another to the left by an elongated neck-like constriction
composed of their own substance—serpentine.

Undoubtedly there also occur bodies having no relation to either
the “ definite shapes” or the “‘ chamber-casts.” We, too; have seen
examples in Grenville Ophite “ of a.mode of communication, of the
chambers when they are completely separated, which,” in certain
aspects, appears to “have its exact parallel in Cycloclypeus :’”’ it con-
sists of thickish, pale-grey, translucent, parallel-sided pieces, with
a subdued silky lustre, stretching across the decalcified passages, and
connecting opposite “‘ chamber-casts,” asin Pl. XIV. fig.10, magnified
105 diameters. When these pieces were first detected, we had no
doubt whatever of their being true “ casts of stolon-passages ;” but
afterwards, on a rigid reexamination, we found every one of them to
be nothing more than a flattened or table-shaped crystal of what
appears to be pyrosclerite* placed edgeways or perpendicular to the
plane of section, and wedged in between two granules. ‘The total
distinctiveness of the former from the latter, a circumstance incon-
sistent with their being “ casts of stolon-passages,” is unmistakeably
marked by their colour, lustre, and well-defined terminations. It
thus becomes evident that the position of these crystals had misled
us (and we may be allowed to suggest this to have been the case
with other investigators), and that certain of the “ narrow passages ”
which have been regarded as “ ewactly corresponding to those in
Cycloclypeus” are not so; for instead of being cylindrical, like the
“canals” represented in figures of this foraminifer, they are broad,
fiat, and parallel-sided. In numerous instances the crystals of pyro-
sclerite extend only partially across the passages, ‘“‘ forming mere
tongues,” which have been misconceived to ‘‘ represent correspond-
ing extensions of the sarcode-body”’ +. When two or more crystals
are associated and lie parallel to one another, or when a single
crystal is divided. by cleavage-partings, we are strongly reminded of
the example represented in the ‘ Quarterly Journal of the Geological
Society,’ vol. xxi. pl. vu. fig. 2. In some cases, a “ white amorphous
mass,” rudely laminated, as in Pl. XIV. fig. 11, magnified 105 dia-
meters, 1s interposed between a crystal and a granule, linking*the two
together.

We have also seen similarly flattened crystals fixed in the calcite
of incompletely decalcified passages. Crystals of the same mineral,
occurring under precisely similar circumstances, characterize the
Ophite from Glanochan and other Connemara localities ; also nume-
rous tabular crystals of mica.. Crystals of chlorite, occupying the
same situation, occur numerously in the Indian Ophite.

* Pyrosclerite or white chlorite, a hydrous silicate of magnesia and alumina,
occurs both amorphous and crystallized. Dana describes it as ‘“ hexagonal(?),”
and having a “ perfect basal cleavage.” The crystals noticed in the text might
be considered to be modified rhombic tables: they are translucent, of a pale
greenish colour, have a weak lustre, and show a transverse lamellar cleavage.
We took them at. first for crystals of some kind of mica; but their lustre is not
sufficiently glistening. Amorphous pyrosclerite, in large lumps, occurs near the
Barna-Oran Ophite-quarry (Connemara). ‘This variety was analyzed by one of
us a few years ago. (See British Association Report for 1860, Sect. pp. 71, 72.)

t Carpenter, Quart. Journ. Geol. Soc. vol. xxi. p. 62,

1866.] KING AND ROWNEY—“‘ EOZOONAL ROCK.” 209

VII. “ Sarcode-chambers.”’

As already noticed, the granules considered to represent these parts
are simulated by wavellite. The same may be said of prehnite and
several other minerals. The imbedded aggregations of garnet and
leucite may be regarded as modified examples. We often find a
close resemblance between them and the concretions of native copper
in porphyry from Canada, of olivine in lava from the Ponza Islands,
and of small zeolitic kernels in amygdaloidal trap. The crystalloids
of pargasite, whether imbedded in calcite or in wollastonite, are even
closer parallels. The isolated grains of coccolite, diopside, and other
minerals, in Tyree marble, are strictly analogous to the large gra-
nules of serpentine isolately dispersed through the calcite of some
specimens of Ophite from Lisoughter*. Chondrodite frequently
affords cases identical in every respect with the ‘‘ chamber-casts :”
specimens of this mineral from New Jersey are common in a finely
granular state: the grains, which are imbedded in calcite, press
closely against one another, their individuality being defined only by
faint segmentations; or, lying more or less apart, they are either
completely separated or attached to one another by stolon-lke necks
of varying lengths.

The characters and circumstances of condition of chondrodite, when
if occurs as just mentioned, are so similar to those displayed by
serpentine in some varieties of “ eozoonal”’ Ophite, especially the one
examined by us from the State of Delaware (also the variety re-
presented in figure 13, Pl. XV., from Lisoughter, in which the gra-
nules are large, often isolated, and unusually wide apart), that it is
impossible to resist believing in the complete genetic identity of the
two minerals. Nay, carry the examination as far as it is possible,
we feel certain that the result will be a full and unqualified surrender
to this belief. If, as Dr. Dawson observes, the granules of serpen-
tine in Grenville Ophite have ‘‘no appearance of concretionary struc-
ture,” certainly the same must be said of the grains of chondrodite,
pargasite, and coccolite in the precited cases. Moreover, if it be ad-
mitted that the former are “casts of sarcode-chambers,” the same
admission must be made with respect to the latter.

Sir William Logan has noticed two remarkable varieties of ‘eozoonal rock,”
identical with Ophite in structure, but differing from it mineralogically. In
one of them, occurring at Burgess, the granules or plates are composed of dark-
green loganite, and the intervening spaces, or matrix, of dolomite; while in the
other, from the Grand Calumet, the former consist of ‘crystalline white
pyroxene” or diopside, and the latter of calcite. Sir William remarked in 1859,
with reference to these two varieties, that if they ‘are to be regarded as the
result of unaided mineral arrangement, it would seem strange that identical
forms should be derived from minerals of such different composition.” Hence,
also observing their structure to have a resemblance to that of Stromatopora

- rugosa, he was led to suppose both varieties to represent a fossil. (See Geology

of Canada, 1863, pp. 48, 49; and Quart. Journ. Geol. Soc. vol. xxi. p. 48.) At
first sight, we admit, there is some reason for this conclusion; but when it,is
considered. that serpentine and diopside are mutually’pseudomorphous, and that

* Specimens of this rock from other places in Connemara, after having been
immersed for a few hours in dilute hydrochloric acid, are often resolved into a
mass of isolated granules scattered over the bottom of the vessel.

210 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

dolomite and calcite are isomorphous, the mineralogical differences presented
by “ identical forms” become at once scientifically explained. If the opinion of
Gustav Rose be correct, that “serpentine is always a product of alteration ” (see
Chem. and Phys. Geol. vol. ii. p. 417), it would not surprise us that what have been
called ‘‘chamber-casts”’ will, in some cases, be found to consist of pyrallolite,
chondrodite, or “ green pyroxene” '(? pargasite), as, inaddition to diopside, these
minerals, in a finely granular state, arranged in layers and imbedded im calcite,
are often mingled with the serpentine, or its varieties, of this rock in Canada
(see Geology of Canada, 1863, pp. 26, 465, &c.). We may here take up a point
alluded to in the early part of this memoir. In all the specimens of Cornish
Ophite which we have examined, nothing like “ eozoonal” structure has occurred
to us, except in a variety formed principally of saponite. This mineral, in one
of our specimens, is here and there associated with calcite, and in these places
it shows a granular structure as well developed as that characteristic of serpen-
tine. An object-glass magnifying 60 diameters, exhibits the granules as true
“‘chamber-casts,” generally spherical in shape, but occasionally elongated or
cylindrical like those which have occurred to us in “eozoonal” Ophite from
Pennsylvania. They are aggregated in clusters, and defined by deep constrictions
or slight segmentations. They also occur attached to one another by stolon-
like necks. As yet we have failed to detect the asbestiform layer and the “ defi-
nite shapes.” Saponite, if Klaproth’s analysis of it be correct, may be regarded
as an allomorph of pyrosclerite; or, as it contains more water than is allowable
in such a view, it may be a pseudomorph of some other ophitic mineral. But,
whatever may be the origin of these granules of saponite, we leave the question
for further investigation.

With regard to the arrangement of the granules of serpentine in
Ophite, the same differences which they display in this respect obtain
with those of pargasite and other minerals. Crystalloids of the one
named occur irregularly or “acervulinely” scattered through a matrix
of saccharoidal calcite; but they are also known to occur arranged
with more or less parallelism in the same base. And, according to
Sterry Hunt, Canadian Ophite contains chondrodite in grains which
are sometimes so disposed as to mark “the stratification of the rock” *.
It is also added that apatite occurs “‘ with the same banded arrange-
ment.”

Connemara Ophite is certainly in general laminated or banded in a very irre-
gular wavy manner, and difficult to understand, often presenting the most
singular and beautiful delineations. In the early stage of our investigations,
we considered the question as to the origin of the phenomenon to be set at rest
on the view that the rock had resulted from the irregular hummocky growth of
‘“‘eozoon.” But it so happens that the same kind of lamination frequently cha-
racterizes the gneissoid limestones of Connemara. Sir William Logan has given
a representation of a precisely similar case, occurring in the Laurentian rocks
on the river Madawaska (see Geology of Canada, 1863, p. 27), which consists
of highly contorted thin layers of gneiss, included in a thickish bed of limestone,
lying between masses of evenly laminated gneiss.

From the fact that certain minerals, when imbedded in-rocks, often affect a
definite or parallel arrangement, which is remarkably the case in graphic
granite, globular diorite (napoleonite), &c., it is conceivable that some of the
more remarkable cases of lamination presented by Grenville Ophite, instead of
being depositional, are the result of segregation. But whatever view may be
taken as to the cause of the phenomenon in general, it is quite clear, from the’
Madawaska and the like instances, that such a cause is in no way connected
with organic agencies.

Certain rocks, both eruptive and sedimentary, exhibit concretionary
or segregated forms simulating the granules of serpentine. Refer-

* Geology of Canada, 1863, p. 465.

1866. | KING AND ROWNEY—“ EOZOONAL ROCK.” 211

ence has already been made to the cupriferous porpyhry of Canada,
some zeolitic traps, and the olivine-lava of the Ponza Islands. We
shall next refer to a remarkable deposit of sedimentary origin.

Few rocks in the entire series of geological formations present any-
thing like the singular configurations which characterize the Permian
Magnesian Limestone of the neighbourhood of Sunderland*. In
other parts of Durham, as along the coast from Ryhope to Hartle-
pool southward, and from Marsden to near South Shields north-
’ ward, this rock has the ordinary lithological structure—earthy, or
compact, occasionally oolitic, &c.; but im many places on both sides
of the mouth of the Wear, it is more or less crystalline; and
where this is the ease, there are often exhibited the most remarkable
forms—honey-combed, discoidal, mammillated, and hemispherical,
coralloidal, stalactitic, reniform, globular, and botryoidal. Very
frequently the amorphous and the crystalline varieties are intimately
associated, the former serving as a matrix for the latter. Thus
constituted, the rock often displays the most unusual appearances,
especially where the amorphous kind is weathered out—resembling,
as the case may be, massive courses of ruined masonry, reefs of
petrified coral, or beds of brown-rusted shot and cannon-balls.

Like most sedimentary rocks, the Primary especially, the one
under consideration has its beds often very much and continuously
divided by joints, varying extremely in their distance from one
another. The beds, in consequence of this divisional structure and
the frequency of depositional partings, often occur as if consisting of ©
huge quasi-rhombohedral blocks. And it frequently happens that
the crystalline forms, wherever they are numerous in such masses,
are seen to strike indifferently from the planes of jointing and the
planes of bedding: hence it is, that dark-brown branching crystalline
coralloids (imbedded in a lighter-coloured matrix) may be fre- .
quently observed striking inwardly from every face of a block.

Where the beds are not divided by jointing, large and small
mammillary and stalactitic forms may often be seen shooting off,
both upwards and downwards, base to base, from two adjacent
planes of bedding, the law of gravitation having been altogether
_ discarded by the mysterious agent which produced them.

From various analyses of the rock, it has been ascertained that
the configurations are composed of carbonate of lime, and that the
matrix consists (as is also the case with the associated ordinary lime-
stones) of carbonate of lime and magnesia. It is therefore highly
probable that the absence of the magnesian constituent in the con-
figurations is not an original condition, but the result of some kind
of segregative action: and it would seem that the agent which
produced this result had gained admission into the very heart of the
beds through their joints and depositional partings, indifferently

_ * These configurations ’werej first described by Professor Sedgwick, in his
classical memoir “On the Geological Relations and Internal Structure of the
Magnesian Limestone,” &c., published in the ‘Transactions of the Geological
Society of London,’ 2nd ser. vol. iti. 1826-1828. They have also been described
by one of us in the “ Introduction” to the ‘Monograph of the Permian Fossils
of England,’ 1850, . ;

212 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

acting transversely to the planes of the one or of the other, thereby
metamorphosing the rock to the extent of thoroughly crystallizing
it, and even in many cases producing a lamination often honey-
combed perpendicular to its bedding.

But what is of special importance, as bearing on the subject of the
present memoir, is the complete similarity existing between many of
the configurations, and the granules and plates of serpentine, in
shape, mutual attachment, and arrangement.

Building Hill, near Sunderland, affords (at least this was the case
some years ago, before it was converted into the People’s Park) in-
numerable specimens of the globular and botryoidal kinds, which,
when cleared of the earthy matrix, are perfect imitations, on a
gigantic scale, of the “‘chamber-casts,” in their form and “acervuline”
arrangement*. We have given a representation in fig. 18, Pl. XV.,
‘of a specimen freed of its matrix, collected many years ago, with-
out, of course, any reference to the question at issue. Its general
resemblance to decalcified specimens of Ophite, where there is an
association of “‘ acervuline ” and laminar “ growths,”’ cannot but be
admitted to be most striking.

But not only do the configurations simulate the forms and ar-
rangement of the granules and plates of serpentine; they equally
simulate and illustrate the “definite shapes.” Specimens may be
procured presenting dendritic ramifications, or a sheaf-like divergence,
or appearing like solid bunches of rounded forms, composed of car-
bonate of lime, and imbedded in or penetrating the calcareo-mag-
nesian matrix, just asthe hydro-silicated magnesian “definite shapes,”
and imitations of a “ sailor’s swab,” occur in the calcareous septa of
“‘eozoonal” rocks. Reduced to microscopic dimensions, many of
them would resemble certain of the structures represented by Daw-
son t, Carpenterz, and Jones§.

VILL. “ Intermediate Skeleton.”

Already sufficient has been stated to show that this part is com-
pletely paralleled by the matrix of certain minerals. The saccha-
roidal calcareous gangues of chondrodite and pargasite closely cor-
respond to the “‘ skeleton,” as it exists in “ eozoonal” Ophite from the
State of Delaware, and in specimens we have collected at Barna
Oran and Lisoughter: in the rocks alluded to the septa exceed in
width the diameter of the granules||. The matrix of bowenite from
Rhode Island, and that of metaxite from Reichenstein, also the sac-
charoidal calcite of the coccolite marble of Tyree, may be adduced
as other instances in point.

The part under notice passes into the layers and beds of saccha-

* An association of the kind is shown in the coloured plate accompanying
Dr. Carpenter’s paper in the ‘Intellectual Observer.’

+ Quart. Journ. Geol. Soc. vol. xxi. pl. vii. fig. 3 (a, a).

+ Ibid. vol. xxi. pl. viii. fig. 5 6, and pl. ix. figs. 5a, b, c,d; also ‘Intellectual
Observer,’ vol. vii. ‘‘uncoloured plate,” fig. 3.

§ Popular Science Review, vol. iv. pl. xv. figs. 5, 6,7, and 8.

|| Is not this the case occasionally in Burgess Ophite? its septa being “in
some parts more than 3'0 millimetres in thickness” (Hunt, Quart. Journ. Geol.

Soc. vol. xxi. p. 69).

1866. | KING AND ROWNEY—‘ EOZOONAL ROCK.” 213

roidal marble associated with Ophite in Connemara. In our days of
implicit belief, we naturally considered that these masses were reefs
of “‘eozoon,” its “‘sarcode-chambers” having got filled with calcare-
ous instead of hydro-silicated magnesian infiltrations—or that they
were accumulations of its disintegrated “skeleton.” But our sub-
sequent decalcifications and microscopic observations completely
failed in revealing the least vestige of foraminiferal structure. We
detected imbedded crystalline tufts, more or less agreeing with those
in the decalcified passages of Ophite, but no traces of ‘ sarcode-cham-
bers ” or their “ proper wall.” We felt perplexed at this unlooked-
for absence of confirmatory evidence: in those days, however, our
scepticism was only dawning.

The “intermediate skeleton” of both Canadian and Connemara
Ophite, when partially dissolved out, besides exhibiting the crystal-
line aggregations, shows what appears under a low power to be
white granular matter scattered over its surfaces, but which, under
a power above 100 diameters, is resolved into minute, short, slender,
bluntish, filiform crystals, generally simple, rarely branching, twist-
ing, leaning, erect, or crooked—in the latter state appearing as if un-
able to hold themselves in an upright position; they stand separated
from one another, or are packed together, forming bundles or lumps
—the latter semitransparent, and of a granular-crystalline structure.
The lumps, like the “amorphous masses,” often block up the de-
calcified passages; and they are intersected by well-developed
cleavage-partings, which appear to agree with those of diopside.
We have observed the filiform crystals disposed in lines, conforming
to the cleavage-partings of their imbedding calcite ; and in this way
they form plates, which, from occasionally connecting opposite
granules of serpentine, we have little doubt have been taken for
“casts of stolon-passages.” Alphonse Gages has evidently detected
the same things in dolomite from Miask.

The filiform crystals, the bundles and lumps, and also the “ amor-
phous masses ” supposed to represent the “ canal-system,” as well as
the occasional coassociation of crystals of pyrites and fragments of
what appears to be titaniferous iron—the occurrence of all these
bodies in the “skeleton” shows that this part is far from being
“‘uniform and homogeneous” as conceived by Dr. Dawson. This
point, however, we do not regard as of much importance ; itis merely
introduced to show that if the organic origin of the calcareous septa
depended on the absence of foreign substances, their presence in these
parts must be accepted as supporting the opposite view.

IX. Geological Considerations bearing on the nature of —
“* Hozoonal” Ophite.

- There yet remains another class of evidences to be considered.
Rocks more or less agreeing with “ eozoonal” Ophite occur, not only
in the Laurentian system, but in others representing widely sepa-
rated geological periods. The “ more abundant” masses of Ophite
found in the “ Quebec series” or Upper Cambrian system are ap-
parently “eozoonal,” being described as “granular” and “ fine-

214 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

grained” *, The Delaware Ophite has indisputably the essential
characters of the type rock; and, considering that its locality lies
somewhat in the direction of the strike of the “Quebec series” in
eastern Canada, there is some probability of this variety being
systemally contemporaneous with the former.

The Connemara Ophite is considered to be Lower Silurian by Sir
Roderick Murchison and Professor Harkness ; but there are reasons
which weigh with us, as already stated, in assigning it to the Lower
Cambrian period. With regard to the varieties from India and
. Bavaria, we are unable to offer any opinion as to their geological
age. A “remarkable ” Ophite, occurring in the Devonian system
at Syracuse in the State of New York, is described as consisting of
an ‘“‘ageregation of grains,”’—a character which leads us to infer
that it is “‘ eozoonal”. The Isle-of-Skye Ophite, which unmistake-
ably possesses the leading features of the Grenville type, brings us to a
much more recent systemal period, it being no other than Liassic!

The fact of ‘“‘eozoonal rock” being a member of various Lower
Primary systems is enough to throw considerable doubt on its pre-
sumed organic origin. The Devonian example at Syracuse, if it
be of the same kind, is a still greater stumblingblockt. But how
are we to explain the presence of “eozoonal” Ophite among the
Liassic saccharoid marbles of Strath, m the Isle of Skye$ ? The bare
fact of the existence of such a rock, separated as its epoch is by
several vast systemal periods from that occurring at Grenville, must
be regarded as a conclusive argument against the view we are op-
posing. But when it is considered that the so called «‘ Kozoon ” has
never yet been found except in metamorphic rocks—that there are

~*® See ‘ Geology of Canada,’ 1863, pp. 248, 266, 611, and 824. The Laurentian
or Grenville Ophite appears, in comparison with that belonging to the “ Quebec
series,’ to occur on a much less extensive scale, forming very subordinate portions
in masses of pyroxene, and zones of limestone (op. cz. p. 25; Quart. Journ.
Geol. Soc. vol. xxi. p. 50, &.). Even the Connemara Ophite seems to be more
abundantly developed and less fragmentary than the latter.

t See Vanuxem, ‘Geology of New York,’ vol. iii. p. 109; also ‘Geology of
Canada,’ 1863, p. 635. .

+ If this Ophite is an “example of local metamorphism,” and it possesses
“eozoonal” structure, it may be held as another geological evidence totally sub-
yersive of the organic origin of the Grenville rock.

§ It is only fair to mention that Professor Harkness, to whom we are indebted
for a specimen of the Isle-of-Skye Ophite, first brought this point under our
notice, when he was with us in Connemara. But at that time, although Dr.
Maculloch, as far back as 1819, had expressed himself “inclined to attribute
the whole metamorphism of the Liassic beds of Strath to the influence of
the Syenite”’ with which they are in contact (see ‘ Western Isles of Scotland,’
vol. i. p. 331), we entertained considerable doubts, countenanced by Sterry Hunt’s
opinion that the hypersthenites around Lough Coruisk belong to the Upper
Laurentian or Labrador system (See Silliman’s Journal, 2nd ser. vol. xxxvi.
p- 226), of the metamorphosed beds above noticed being Liassic. Now, what-
ever may be the age of the neighbouring hypersthenites, all our doubts have been
dispelled regarding the chronology of the saccharoid marbles, and their included
layers of Ophite, after reading Geikie’s paper “On the geology of Strath, Skye,”
as this author, with Dr. Wright’s palzontological assistance, has clearly shown
them to be altered limestones, shales, and grits of the Liassic period (See Quart.
Journ. Geol. Soc. vol. xiv. pp. 1-36).

1866. ] KING AND ROWNEY—“ EOZOONAL ROCK.” 215

miles in thickness of primary wnaltered calcareous argillaceous and
mixed deposits in which no vestige of this “ fossil” has been found,
and in which its occurrence ought to be certain, had it been a fora-
miniferal organisim,—we shall be much surprised if, with such plain,
simple, and elementary facts before him, this ‘creature of the dawn”
—the “oldest type of organic life yet known ”—does not soon be-
come to the geologist a memorable nonentity.

X. Summary.

Although zealous advocates at one time for the organic origin of .
“‘ eozoonal” Ophite, we now, after a prolonged investigation, and
after, as we believe, leaving no point unnoticed, feel ourselves under
. the necessity of totally relinquishing that opinion.

It has been seen (1) that the “‘ chamber-casts” or granules of ser-
pentine are more or less simulated by chondrodite, coccolite, parga-
site, &c., also by the botryoidal configurations common in Permian
Magnesian Limestone; (2) that the “intermediate skeleton” is
closely represented, both in chemical composition and other condi-
tions, by the matrix of the above and other minerals; (3) that the
‘proper wall” is structurally identical with the asbestiform layer
which frequently invests the grains of chondrodite—that, instead of
belonging to the skeleton, as must be the case on the eozoonal view,
it is altogether independent of that part, and forms, on the contrary,
an integral portion of the serpentine constituting the “ chamber-
casts,” under the allomorphic form of chrysotile—and that perfectly
genuine specimens of it, completely simulating casts of separated
nummuline tubules, occur in true fissures of the serpentine-granules ;
(4) that the “ canal-system” is analogous to the imbedded crystal-
lizations of native silver and other similarly conditioned minerals,
also to the coralloids imbedded in Permian Magnesian Limestone—that
its typical Grenville form occurs as metaxite, a chemically identical
mineral imbedded in saccharoidal calcite ; (5) that the type examples
of “casts of stolon-passages ” are isolated crystals apparently of py-
rosclerite. Furthermore, considering that there has been a complete
failure to explain the characters of the so-called internal casts of
the “‘ pseudopodial tubules ” and other “ passages ” on the hypothesis
of ordinary mechanical or chemical infiltration, also bearmg in mind
the significant fact that the ‘‘intermediate skeleton,” in Irish and
other varieties of “eozoonal rock,” contains modified examples of the
“definite shapes” more or less resembling the crystalline aggrega-
tions and prismatic lumps in primary saccharoidal marbles—that
*“‘eozoonal” structure is only found in metamorphic rocks belonging to
widely separated geological systems, never in their unaltered sedi-
mentary deposits,—taking all these points into consideration, also the
arguments and other evidences contained in the present memoir,
we feel the conclusion to be fully established, that every one of
the specialities which have been diagnosed for ‘‘ Hozoon Canadense ”
is solely and purely of crystalline origin: in short, we hold, without
the least reservation, that, from every available standing point—
foraminiferal, mineralogical, chemical, and geological—the opposite
view has been shown to be utterly untenable.

216 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

XI. Conclusion.

From what has been stated in some of the preceding pages,
respecting the various chemical changes which “ eozoonal” Ophite
appears to have undergone, and its mineralogical constituents, we
are strongly inclined to believe that it is a pseudomorphic rock, that
it existed at one time in the ordinary metamorphic state, perhaps as
hornblendic or augitic gneiss, and that it is primarily of sedimentary
origin*., Whether the same may be concluded of all ophitic rocks is:
a question on which we cannot offer any opinion—negative, or affir-
mative. There are some grounds for believing, however, that certain
dolerites, generally considered to be of eruptive origin, have become
changed into Ophite: and though we have not detected any “eozoonal”
structure in an example apparently of the kind, from Monzoni in the
Tyrol, which has fallen under our observation, it would not surprise
us if this structure were found in ophitic rocks supposed to belong
to the eruptive section, considering that the essential mineral (augite)
of dolerite contains a large percentage of silicate of lime+.

_ * Dr. Sterry Hunt states that ‘‘pseudomorphism, which is the change of one
mineral species into another by the introduction or the elimination of some ele-
ment or elements, presupposes metamorphism, since only definite mineral species
can be subject to this process” (see Journal of the Geological Soc. of Dublin, vol.
x. p. 88). We accept this view of pseudomorphism ; but we see no reason why
the change can only have “taken place in some mineral species, in veins, and
near the surface’””—why it cannot have operated on a sufficiently extensive scale
to generate the layers and beds of Ophite interstratified with the Laurentian
limestones and gneiss of Canada. It may be, that “ the alteration of great masses
of silicated rocks by such a process is as yet an unproved hypothesis: we
cannot but think, however, that Dr. Hunt has insufficiently estimated the evidence
which may be adduced in its favour. One which we shall now cite seems to
bear us out in this idea: alluding to Blum’s discovery of pseudomorphs of ser-
pentine after augite, at Monzoni, Bischof expressly states, ‘it is not merely the
fine crystals, which occur in its drusy cavities and fissures, that are changed, but:
the whole mass of the rock is converted into serpentine” (See Chem. and Phys.
Geology, vol. 11. p. 322).

t Sir Charles Lyell has stated that ‘‘ even if we had not discovered the Hozoon,
we might fairly have inferred” that the ‘“ calcareous masses, from 400 to 1000
feet and more in thickness,” associated with it ‘were originally of organic
origin”’ (Elements of Geology, 6th edition, p. 580). Now, whatever the “ cal-
careous masses” may have originated from, the idea of their being “eozoonal”
must be abandoned. We do not dispute the above inference, which, be it con-
sidered, does not necessarily involve animal agency alone, as such ‘“ masses”
may be the debris of calciphytes, like the calcareous accumulations still abun-
dant on many of our present sea-bottoms and resulting from the growth and
decay of various kinds of nullipores. But it may turn out that they are not of
organic origin at all. Doubtless some, calling to mind the beds of travertine oc-
curring at Rome, may be disposed to regard them as of chemical origin. Another
idea, however, strikes us just now. Feeling confident in the view herein taken
of the origin of ‘“ eozoonal”” Ophite, we are strongly inclined to believe that its
calcareous portions are segregations derived partly, or wholly, from the silicate
of lime contained in hornblendic or augitic rocks, such silicate having been con-
verted into a carbonate by the introduction of water containing free or combined
carbonic acid. (In lime-magnesia augite, as diopside, these bases, important in
“‘eozoonal”’ Ophite, amount to about 43 per cent.) There are some grounds for
believing that the lenticular masses of saccharoidal calcite, or “‘ primary” marble,
often imbedded in metamorphic rocks, have originated in the same way. But
whether the vast “ calcareous masses,” referred to by Lyell, are of pseudomorphic
origin is a question on which it behoves us to speak with less confidence ; at any
rate, such a view, as will now be seen, ought to command due consideration.

1866.]

Fig. 1.

cr

KING AND ROWNEY—‘** EOZOONAL ROCK.” 217

EXPLANATIONS OF PLATES XIV. & XV.
Illustrative of the view of the inorganic nature of Kozoon.

Puate XIV.

Section, viewed as an opaque object, of a portion of a granule (‘‘ chamber-
cast’’) of serpentine, having one edge, facing a decalcified passage,
furnished with two asbestiform layers. The inner layer is perfectly
compact, except at the left end; the outer one has the fibres in the
left half standing apart, but in the right half they are in close contact.
The outer layer is nearly separated from the inner one. The granule
is green and translucent; the layers are white and vitreous. Mag-
nified 210 diameters. From Grenville.

. Section, viewed as an opaque object, embracing a lobulated granule of

green serpentine, and a portion of its matrix (lower part), com-
posed of white saccharoidal calcite; the specimen is not decalcified.
The striated portion represents the asbestiform layer (“‘ pseudopodial”
or “proper wall”), which is perfectly compact, except at the places
marked a and 8, in which the fibrous structure is in an intermittent or
incipient state of development. The peculiarities of its structure show
that the layer is an integral portion of the serpentine. Magnified 210
diameters. The specimen has been examined with a power of 350,
with the same result. From Grenville.

. Section, viewed as a transparent object, of three granules of serpentine

(“‘chamber-casts”), with their edges notched or broken up into sepa-
rated bundles of asbestiform fibre. The interspaces between the
bundles, as well as those between the granules, are filled with flocculent
matter, Our view of the specimen is, that the spaces between the
bundles of asbestiform fibre originally consisted of serpentine, which has
been converted into flocculite ; also, that possibly the entire mass of the
latter between the granules was once serpentine. Magnified 120 dia-
meters. ‘The specimen has also been examined as an opaque object,
under a power of 350, with the same result. From Grenville.

. Section, viewed as an opaque object, representing a small portion of a

long fissure, which intersects a number of granules of serpentine. One
of the walls of the fissure is crowded with aczeulé (¢dentical with
“casts of pseudopodial tubuli” of “ Hozoon Canadense”), separated,
as well as in close contact: in a few places the acicult form bundles ;
see centre of the lower wall. The upper wall is crowded with a very
thin asbestiform layer. Magnified 110 diameters. From Lisoughter.

. Section, viewed as an opaque object, of a portion of asbestiform layer

(identical with that of “ Hozoon Canadense”), lying between, and
attached to, two grains of yellowish-brown chondrodite, In the left
half, the layer, which is white, translucent, and silky, is perfectly
compact; but inthe other half, its fibres are in some places separated
and a little twisted. Magnified 120 diameters. From New Jersey.

. Section, viewed as an opaque object, of grains of chondrodite separated

by an asbestiform layer, the fibres of which are here and there apart,
and in some places not strictly parallel. Magnified 60 diameters.
From New Jersey.

. A grain of chondrodite, viewed as an opaque object. It is furnished at.

one end with the remains of an asbestiform layer, the fibres of which
form slender aciculi; or, in other words, the aciculi are composed of
asbestiform fibre. The vacant spaces appear to have been occupied by
fibres or aciculi, which, through some cause have disappeared. Mag-
nified 120 diameters. From New Jersey.

. Section, viewed as an opaque object, of a granule (“chamber-cast”’) of

serpentine, showing a fringe of asbestiform layer (‘‘tubulated proper
wall”’), which generally consists of parallel fibres; but in some places
the fibres are divergent. In one place the layer is replaced by a coat
of flocculite. It is our opinion that the latter has resulted from a
change either of the asbestiform layer or of the serpentine. Magnified

VOL. XXII.— PART I, R

218

Fig. 9.

10.

ie

13.

14,

15.
16.

is

18.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

210 diameters. From Lisoughter. (The figure is represented more
compressed than it really is,so asto occupy as little space as possible.)

This figure represents, by reflected light, a mass of flocculite lying be-
tween, or adjacent to, two granules of serpentine. One of the granules
is fringed with aciculi. 'The flocculite shows here and there a rude
divisional or prismatic structure, which becomes acicular ; in two places
well-developed aciculi rise out of the mass. Magnified 210 diameters.
From Lisoughter.

Two granules (‘‘chamber-casts”), viewed by reflected light, of serpentine
connected by a crystal of pyrosclerite? (answering to a “cast of a
stolon-passage’’), lying across a decalcified passage. ‘The crystal has
a thin layer of white granular matter adhering to each of its sides;
and the granules are furnished with a portion of asbestiform layer.
Magnified 105 diameters. From Grenville. —

Crystal of pyrosclerite (?), answering to a “cast of a stolon-passage,”
lying across a decalcified passage; it is not long enough to connect
two opposite granules of serpentine, but the connexion is completed
by the interposition of a ‘“‘ white amorphous mass,” 0, rudely lami-
nated. The other connecting body, which may also be taken for a
“cast of a stolon-passage,” consists entirely of a rudely laminated
‘white amorphous mass.” Magnified 105 diameters. From Grenville.

Puate XV.

2, This figure represents a dendritic specimen of metaxite (¢dentical with re-

presentatives of the “canal-system” of “ Hozoon Canadense”), as it ap-
pears under an object-glass magnifying 110 diameters. Obtained by de-
calcifying its matrix—saccharoidal calcite. From Reichenstein, Silesia.

A small portion of Ophite, decalcified, from Lisoughter. The spheroidal
bodies are granules (“ chamber-casts” of ‘‘ Hozoon”) of translucent ser-
pentine, imbedded in saccharoidal calcite (‘‘ skeleton” )—the dark por-
tions. Tufts of crystals (‘‘metamorphosed” examples of the “ canal-
system”’) are variously attached to the granules, while other tufts are
fixed in the calcite. ‘Two granules in the middle of the lower portion
of the figure are connected by three white, slightly granular, parallel
plates, representing ‘“stolon-passages;” other granules are connected
by tufts of crystals. Magnified 25 diameters.

Granule of serpentine (“‘chamber-cast”’), from a decalcified specimen of
Lisoughter Ophite, to which are attached scopiform bundles of crystals,
representing “ metamorphosed” examples of the “ canal-system.”’ The
crystals are divergent, also subparallel. Magnified 210 diameters.

Represents the two granules of serpentine noticed under figure 13.
Magnified 120 diameters.

Representations of a’ branching vermicular body, a, lying lengthways,
and of a transverse’ section of another, 6, both showing acicul
shooting off from their surfaces. The vermicules and aciculi, of a
yellowish-brown colour, are imbedded in transparent chalcedony.
Magnified 210 diameters. From a “ Moss-agate” presented by Pro-
fessor Tennant. .

An ‘‘amorphous mass,” representing the ‘canal-system,” of a prismatic
structure, lying in a decalcified passage, c, between four irregular-
shaped granules of serpentine, a. The “mass,” 0, at its sides, is sepa-
rated into prisms, which curve off, and in a few places become
branched ; it is, for the most part, however, compactly prismatic, and
has an incipient lustre.’ “Magnified 60 diameters. From Grenville.

Representation, natural size; of a botryoidal specimen of Permian lime-
stone, from Building Hill (People’s Park), near Sunderland. The
rounded and irregular-shaped bodies, formed of brown subcrystalline
carbonate of lime, s¢mulate the ‘ chamber-casts” of “‘Hozoon Cana-
dense:” -the vacant spaces, once filled with earthy carbonate of lime
and magnesia (which has been weathered out), correspond to the

- decalcifiedpassages or the so-called ‘calcareous skeleton.”

Quart Journ Geol. Soe Vol XXII-P1 XV.

Sate Sndin.ne

)

|

“2h

F 2
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avy |

C

M.&N Han

Quart Journ.Geol.Sec Val. XXII, Pl, XIV.

YA

FM Wilhams PLS. F.Z.8 lth. | M.&NHanhart imp

BOAO@ONAL ROCKS .

1866. ] CARPENTER—EOZOON CANADENSE. 219

2. Supprementat Nores on the Structure and AFFINITIES of Kozoon
CanapEensk. By Witttam B. Carrenter, M.D., F.R.S., F.G.S.

Stnoz the date of my communication to the Geological Society made
through Sir William Logan, upon the remarkable fossil discovered
by him in the Laurentian rocks of Canada, I have given a consider-
able amount of time and attention to the further investigation of its
characters; and I am desirous of recording certain additional fea-
tures in its structure, which seem to me to strengthen the view ori-
ginally put forward by Dr. Dawson, and confirmed by my own in-
quiries, of its Foraminiferal affinities.

It will be remembered that this view was originally propounded
by Dr. Dawson as the result of his investigations (1) into the re-
lations of the calcareous and siliceous layers, which appeared to him
to indicate that a chambered calcareous skeleton had been in-
filtrated by silicates in solution, so as to leave a siliceous * deposit
in the spaces previously occupied by the animal body; and (2) into
the distribution of an arborescent “ canal-system” which he de-
tected in the calcareous skeleton, bearing a most remarkable re-
semblance to the canal-system described by myself in Calcarinat.

My own observations upon the specimens placed in my hands by
Sir W. Logan supplied an important confirmation to this view, for
these disclosed the fact that the proper wall of the chambers, when
well preserved, exhibits the finely tubular structure of the Num-
muline Foraminifera; which is demonstrable as well in thin
transparent sections{, as in decalcified specimens, which show the
siliceous casts of the interior of the chambers to be covered with a
thin ‘‘ asbestiform layer” composed of acicular fibres standing upon
end, usually parallel to each other§. These fibres I regard as the.
internal casts of the tubuli of the shelly layer, which were originally
occupied by minute filaments (pseudopodia) proceeding from the
sarcodic body of the animal. And I feel justified in doing so by the
fact that a recent siliceous cast of an Amphistegina from which the
shell has been removed by decalcification, kindly presented to me by
my friend Mr. W. K. Parker, affords a perfect representation of this
“‘ asbestiform layer”—the only difference being that the fibres are
- larger and more separate, in accordance with the characteristic
tubulation of the shell in this genus. This cast gives a perfect
model in a green silicate (glauconite?) of the lobes of the body, of the
canal-system, and of the tubuli of the shell-wall; and as the shell
within which it was formed was brought up with many similar ones
by Mr. Jukes in his dredgings on the Australian coast, it is obvious
that the complete replacement of the segments of the animal body

* T use the term siliceous, here and elsewhere, to mean compounds of which

silicic acid is the characteristic ingredient. :
Compare Dr. Dawson’s delineations of the canal-system of Hozoon Cana-

dense, in Quart. Journ. Geol. Soc. vol. xxi. Plate vii. figs. 3 (a a) and 5, with
the representations of the canal-system of Calcarina in my ‘Introduction to
the study of the Foraminifera,’ Plate, xiv. figs. 4, 8, 9.

{ Quart. Journ. Geol. Soc. vol. xxi. Plate viii. figs. 44,40. .

§ Op. cit. Plate ix. fig. 4.

R 2

220 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

and of their minute filamentous prolongations, by a siliceous deposit
in the cavities and tubes which they occupied, was effected by some
process at present in operation upon thesea-bottom. And whatever
view we may take of the nature of this process,—whether we suppose
these chambers and tubes to have filled when empty by infiltration,
or regard the animal matter which originally occupied them to have
given place to the siliceous deposit by a process of chemical sub-
stitution* ,—the fact remains, that an undoubted internal cast of a
recent Foraminifer presents the exact parallel to the model of the
animal body of Hozoon obtained by the removal of its calcareous
skeleton. Indeed it was in consequence of the suggestion afforded
by this specimen of Amphistegina, that I was led to look for the
corresponding structure in the decalcified Hozoon; the discovery of
which affords no slight confirmation of the view previously arrived
at by the examination of thin transparent sections.

My observations upon the Nummuline structure of the proper walls
of the chambers have been fully confirmed by Dr. Dawson, who
thus speaks in an Appendix to the Canadian reprint of his paper on
Eozoon. <‘ Since the above was published, I have had opportunities
of examining slices and decalcified specimens of Hozoon from Petite
Nation, the locality which afforded the specimens referred to by
Dr. Carpenter ; and I have much pleasure in adding my testimony
to his observation of the distinctness of the proper wall of the
chambers from the supplemental or intermediate skeleton, as ex-
hibited in these specimens.” :

This Nummuline tubulated structure comes to be of special im-
portance, now that the organic nature of the Eozoic serpentine-
limestone has been formally called in question. For even if it be
admitted that the peculiar arrangement of the calcareous and siliceous
components of the Kozoic limestone, and the remarkable dendritic
passages hollowed out in the calcareous layers, are capable of being

* Notwithstanding that this idea has been designated by Profs. King and
Rowney as so completely destitute of the characters of a scientific hypothesis as
to be wholly unworthy of consideration, I believe it to be the one commonly
entertained by those who have given most thought to the mode in which the si-
licification of Woods and of the soft tissues of Sponges and other organisms has ©
been effected, so as to preserve the minutest features of their structures. And
those eminent geologists who were present with me at the discussion which took
place in Paris upon the subject of the Abbeville Jaw, will recollect that no less
an authority than Prof. Milne-Edwards stated that he believed that infiltration
of bones and teeth was more likely to take place when their cavities were occu-
pied by animal matter at the time they were imbedded, than when those cavities
had been emptied by its decay ; the minute tubuli being, in his view, more readily
and completely filled by the process of substitution, during the decomposition of
their animal contents, than they could be by mere percolation. ‘This suggestion
was thrown out to account for the fact mentioned by M. Lartet, that completely
infiltrated and non-injiltrated bones are often found in the same stalagmitic
deposit. My own early investigations into the structure of Nummulites had long
before led me to the conclusion that among those found imbedded in the clay
of Bracklesham Bay, the specimens most completely infiltrated with carbonate
of lime had their chambers occupied with animal matter at the time when this
fossilizing process commenced (see Quart. Journ. Geol. Soe. vol. vi. p. 23,
Dee ili. fig. 2); traces of it being distinguishable even to the very centre of
the spire.

ESCG CARPENTER——EOZOON CANADENSE. 221

accounted for by inorganic agencies, there remains the Nummuline
structure of the chamber-walls, to which—I venture confidently to
assert—no parallel can be shown in any undoubted mineral product*.

The “asbestiform layer” obtained by the decalcification of the
Nummuline shell-wall, which sets free the siliceous internal casts
of its tubuli, presents a series of remarkable variations, which can
be closely paralleled by the variations existing in the course of the
tubuli in the shells of living Nummuline Foraminifera. What we
may consider the normal arrangement is the passage of the tubuli
in a straight and parallel course from the internal to the external
surface of the shell-wall; and this is represented in Hozoon by a
regular disposition of the acicular fibres, which stand side by side,
like the filaments that form the pile of velvet, their lower ends resting
on the subjacent segment, whilst their upper form a uniform surface
so close in texture as to be scarcely resolvable into the points of its
constituent aciculit. But, as is often the case in Operculinat, the
tubuli may depart from their normal parallelism, separating from each
other in some parts, and becoming more closely crowded in others ;

* It may be thought a matter for regret that, before putting themselves in a
position of antagonism to those who have made a special study of the minute
structure of Foraminifera, Profs. King and Rowney should not have availed
themselves of the opportunity publicly offered them some months since (see the
‘Reader’ for July 8th, 1865) of inspecting my preparations of Hozoon. I have
recently learned from personal communication with Prof. Rowney, not only
that he had no practical knowledge of the structure of Nnmmuline shells, but
that he had not, until I myself showed them to him, ever seen any transparent
sections of Hozoon thin enough to give a good view of its tubuliferous layer,—
his observations having been almost exclusively made upon decalcified specimens.
And it is obviously from this limitation to one method of inquiry, that Profs.
King and Rowney have fallen into what I feel able to demonstrate to be the
fundamental error of their whole treatment of this part of the subject,—the
assumption that the ‘“‘asbestiform layer” is, iz zts original state, before having
been acted on by acid, a mere bundle of siliceous fibres, instead of being (as I
maintain) a continuous layer of calcareous shell, the vertical tubuli of which
have been filled up by the substitution of siliceous deposit for the threads of
animal matter which originally occupied them. If they had made the experi-
ment, which I have over and over again repeated, of subjecting a very thin
transparent section of Hozoon, cemented on glass by Canada balsam, to the
action of dilute acid, they would have been at once convinced by the complete
alteration in the appearance of this layer, that a transparent substance inter-
vening between the asbestiform fibres and cementing them together, has been dis-
solved out. This becomes still more obvious where the fibres diverge from one
another in some parts and converge in others, as will be described in the next
paragraph.

t It is apparently from this continuity of the external surface of the asbesti-
form layer, that Profs. King and Rowney have been led to the inference that its
fibres are so closely compacted together that there is no room for any intervening
calcareous cement. But if they had been familiar with the study of living
Foraminifera, they would have been aware that the pseudopodia which have
passed through the pores of the shell, coalesce on its external surface into a con-
tinuous layer of sarcode; so that the continuity of the external surface of the
asbestiform layer is precisely what we should expect, if this layer represents the
filamentous extensions of the original sarcode-body of the animal. A still more
remarkable representation of this sarcodic layer in the siliceous model of the
animal of Kozoon will be presently described.

¢ See Memoir on Operculina in the Phil. Trans. for 1859, p.54, and Plate iv.
figs. 2, 4, 11.

222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

so that instead of the uniform punctation which the internal surface
of the chamber-wall exhibits, we may find great diversities in the
disposition of their external orifices, these being often congregated in
bands and clusters, with intervals of non-tubular shell-substance
between them. ‘The same is the case in the recent Amphistegina ;
and the internal cast, or model of its animal, already referred to pre-
sents the same kind of variations in the course of the siliceous threads
which represent the pseudopodia, as those which are exhibited in a
higher degree by the “ asbestiform layer” of Hozoon. For decalcified
specimens of this often show us fissures in the asbestiform layer, re-
sembling those left in the surface of a piece of velvet-pile by doubling
it back; these fissures represent the non-tubular spaces of the shell-
wall, which are left by the convergence of the tubuli in other parts
into bands and tufts. A more marked degree of the same conver-
gence, bringing a large number of the pseudopodia that proceed from
each segment into one bundle, is frequently to be seen in parts in
which there is an unusual development of the intermediate skeleton
and canal-system. And here an additional peculiarity often pre-
sents itself, which is in such remarkable accordance with what I had
previously observed and recorded in the recent Foraminifera to which
Hozoon seems most nearly allied, that it is difficult to conceive that
accordance to be without a meaning. In my description of the canal-
system of Calcarina I had expressed my belief that the usual origin
of the canals of the intermediate skeleton is not from the cavities of
the chambers, but from lacunar spaces intervening between the out-
side of the proper walls of the chambers and the intermediate skeleton
by which they come to be overgrown; and in my previous commu-
nication upon Hozoon (p. 63) I expressed the opinion that the same
was probably the case in that organism. These lacunar spaces, in
the living animal, would be occupied by films of sarcode formed by
the coalescence of the pseudopodia on the external surface of the
proper wall of the chambers; and from these films would pass off
the sarcodic extensions which occupy the canal-sytem. Now in
those varieties of the asbestiform layer which exhibit a foliated or
penicillate arrangement of the silicified threads, the bands or tufts
which the surface of the asbestiform layer then presents are often
connected by plates of the same siliceous material, in which the stems
of the dendritic models of the canal-system are frequently implanted.
And these plates can in many instances be plainly seen to be formed
by the spreading-out of the material which formed the coalesced
bands and tufts; just as the sarcodic layer on the surface of the
living shell is formed by the spreading-out of coalesced bundles of
the pseudopodia that have emerged from the chamber-wall*.

I have thought it desirable to dwell thus fully upon the structure
of the Nummuline chamber-wall, and the parallel between the variety
of appearances which it presents in Hozoon and those exhibited by

* This structure may be what has been described by Profs. King and Rowney
as ‘‘a double asbestiform layer.” If so, its presence, instead of affording an ar-
gument against the Foraminiferal nature of Eozoon, supplies an unexpected
confirmation of that doctrine.

1866.] _ _ CARPENTER——-E0ZOON CANADENSE, 223

recent Foraminifera*, because it is by this feature that the organic
origin of Hozoon is capable of being most unmistakeably recognized.
If my account of it is correct, no more doubt can be reasonably en-
tertained of the animal nature of Hozoon than of the animal nature
of any extinct type of Nummuline Foraminifera; and all the other
curious features of its structure, including the singular varieties in
the distribution of its canal-system, may be accepted without
hesitation.

But even if some undoubtedly mineral product could be shown
to present the characteristic peculiarities of the Nummuline shell-
wall, I should be still prepared to maintain the organic origin of
Hozoon on the broad basis of cumulative evidence afforded by the
combination, in every single mass, of an assemblage of features which
can be only separately paralleled elsewhere ; and in the repetition of
this combination with the most wonderful exactness, over areas of
immense extent. This evidence, indeed, is very much of the same
nature as that on which the doctrine of the Human fabrication of the
« flint implements” is now universally accepted. No one, on-looking
at such an implement, would be justified in saying of any single
fracture presented by its surface, that it mzght not have been acci-
dental ; yet that man must have a strong faith, who could honestly
maintain that any succession of accidental fractures would have been
likely to shape out even a single specimen. But admitting such a
possibility in regard to one, it is narrowed down by every repetition
of the same or of a similar form, to a vanishing point which the
intellect refuses to apprehend.

Although not perhaps entitled to any great weight, yet the an-
tecedent probabilities of the case are not to be disregarded. Geolo-
gists are now, I believe, very generally agreed in the opinion that
all the great beds of limestone in the formations known to be
fossiliferous are the products of animal agency, which separated
carbonate of lime from its solution in the waters of the ocean in the
form of Corals, Shells, Encrinite-skeletons, &c. And it is also fully
admitted that the crystalline condition of a limestone affords no ar-
gument against this view; many comparatively modern rocks, of
whose organic origin there can be no reasonable doubt, having been
brought to this condition by subsequent metamorphism. The,
occurrence of limestone beds in the Laurentian rocks, therefore,
affords a presumption in favour of the existence of marine animal
life at that epoch ; in the same manner as the occurrence of beds of
graphite may be fairly regarded as indicative of the antecedent
existence of vegetation. And while this presumption is in no degree
invalidated by the crystalline condition which usually prevails in
these rocks, it derives additional weight from the fact noticed by Sir

_ * Tt may serve to show the necessity of practical familiarity with the micro-
scopic appearances in question, if I mention the fact, that an eminent Paleon-
tologist who had previously committed himself to the opinion that the Num-
muline layer of Hozoon is simply ‘an agatized mineral,” gave precisely the same
verdict upon a section of a recent Nummuline shell,—thus unintentionally
bearing the strongest testimony to the identity of the two structures, and con-
sequently to the organic nature of the former.

224 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

W. Logan, that some of the Laurentian marbles when struck give
forth the same overpowering smell of carburetted hydrogen, as is well
known to be given, off from many beds of Carboniferous Limestone
whose organic origin is most distinct.

Another probability is afforded by the striking cosemiblaayee ob-
served by Sir W. Logan in the general arrangement of the masses
of Hozoon in Foraminiferal reefs, to the reefs formed by the stony.
Corals; and the evidence of successional building-up of these, as
shown by the disintegration of some parts of what would have been
once the living surface by currents and eddies, which have left cavities
and recesses that were subsequently filled by a new overgrowth.

The alternating succession of calcareous and siliceous lamelle, of
which as many as fifty may be counted in a single mass of Hozoon,
is a feature which if not absolutely without parallel in the inorganic
world, is a very singular one; and the difficulty of accounting for it
is greatly increased when we look upon the vast multitude and the
singular uniformity of its repetitions in the separate masses of Hozoon.
The difficulty is yet further augmented when it is taken into account
that the alternating minerals, though invariably calcareous and sili-
ceous, are not constantly the same; the serpentine being often re-
placed either by pyroxene or by log eanite, and the carbonate of lime
by dolomite. Now on the hy pothesis of organic origin, nothing is
easier than to account for the regular alternation of calcareous and
siliceous layers,—the former representing the original skeleton formed
by successional growth; and the latter representing its chambers,
originally filled with a living sarcode-body, which was subsequently
replaced by siliceous minerals by a process which (whatever its
nature) has been repeated upon the bodies of Foraminifera in every
great geological epoch from the Silurian to the present. And it was
the coexistence of this uniformity in structural arrangement with
diversity in the component minerals, which first impressed upon the
mind of Sir W. Logan the idea of the organic nature of these masses.

The greater variability in the thickness of the calcareous lamelle
than in that of the siliceous, is a point of minor importance, but not
without its relevancy; for it is exactly paralleled among recent
Foraminifera. As Unios and other freshwater mollusks will form
thick or thin shells according to the abundance of Carbonate of Lime
in the water they inhabit, so do we find among the Nummulites of
different localities’ extraordinary diversities of form produced by
variations in the thickness of their shelly layers; the same species
having sometimes a thickness equal to only one third of its diameter,
whilst in other specimens the thickness equals three-fourths of the
diameter,—the dimensions of the chambers being nearly the same
in both cases. The difference in the thickness of the calcareous
layers of Eozoon, on the hypothesis of its organic origin, depends
upon the amount ‘of superficial addition made in the form of “ sup-
plemental ” or “intermediate skeleton” to the proper walls of the
chambers, the cavities of which are represented by the siliceous
layers ; an‘ wherever the interval between two siliceous layers is
unusually wide, an unusual manifestation of the canal-system is

1366. | CARPENTER—-EOZOON CANADENSE. 225

almost sure to present itself. This constant relation between the
development of the “‘ intermediate skeleton” and that of the “ canal-
system ” is in such precise accordance with what I have uniformly
found to exist in Foraminifera*, as to add another fact of no mean
significance to our growing accumulation of evidence.

Having dwelt sufficiently in my former note on the characters which
I regard as essentially Foraminiferal, I need not here do more than
recapitulate them as follows :—1.. The constant segmental division
of the siliceous layers, indicating a series of chambers only partially
divided from each other, as in Carpenteria, but occasionally sepa-
rated completely by interposed calcareous septa. 2. The perforation
of these septa by several passages of communication between the
chambers, as in Cycloclypeust. 3. The substitution of the acervuline
piling-together of the chambers, in the latter stages, for the regularly
storied arrangement of the earlier; a change very common among
Foraminifera. It is further not a little significant that the siliceous
segments in this acervuline portion have the same average dimensions
as those of which the subjacent laminz are composed. The uni-
formity with which the acervuline mode of aggregation succeeds the
' lamellar could scarcely be expected if these masses were of purely
mineral origin. 4. The distinctness of the proper wall of the cham-
bers from the intermediate skeleton; a feature especially charac-
teristic of the higher Foraminifera. 5. The precise conformity in
the structure of the former to that of the Nummuline Foramini-
ferat. 6. The constant proportion between the development of the
latter and that of the canal-system. 7. The correspondence in size
between the elementary parts of Hozoon and those of the Forami-
nifera to which it is most nearly related. This is a feature of no little
importance, when we take into account the extreme variability in the
size of the elementary parts of Mineral aggregations§. It is almost

* Introduction to the study of the Foraminifera, p. 63.

t The explanation of these passages offered by Messrs. King and Rowney, is
based on the representation of them given in the somewhat diagrammatic figure
illustrating my former note (Plate VIII. fig. 2). That it is totally inapplicable
to the case, becomes at once apparent on miscroscopic examination of the large
number of examples I now possess of this very characteristic feature.

{ Itis urged by Profs. King and Rowney as an objection to the Foraminiferal
doctrine, that this supposed tubular wall is found on the under or attached side
of each lamella, as well as on the upper or free surface, and that it is incon-
ceivable that a layer thus perforated for the passage of pseudopodia should be
formed where there is no exit for them. ‘The objection only shows their want
of acquaintance with the fact that many Foraminifera (both recent and fossil),
having perforated shells, habitually grow affixed to seaweeds, corals, shells, &c. ;
and that the attached side possesses the characteristic tubular structure no less
than the free. I believe that in all these cases there intervenes in the living
state a thin layer of sarcode between the shell and the subjacent surface, the
evidence of whose presence*in Mozoon is afforded by the continuous siliceous
lamellz already referred to as often connecting the outer ends of the aciculi of
the asbestiform layer. .

§ The only other objection of any weight advanced by Messrs. King and
Rowney, is the fact that a chambered structure and asbestiform layers are some-
times met with in the midst of the thick purely serpentinous layer which usually
underlies the masses of Hozoon. Now if such be really the fact, it would only
prove the persistence of bands of the original structure in parts which had been

226. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 10,

inconceivable that throughout the enormous masses of Eozoic serpen-
tine, the siliceous segments, if merely concretionary, should never ex-
ceed a minuteness that is rarely encountered among ordinary minerals.

Every one who has been accustomed to attend to the subject of
evidence is well aware that the concurrence of a number of separate
and independent facts, not one of them possessing much probative
value in itself, may lead to a moral certainty scarcely inferior to
that obtained from demonstration. This is the case when the ag-
gregate of these facts is capable of being reconciled with a single
hypothesis, and with that one only, and when the facts can only be
otherwise accounted for by a number of separate hypotheses having
no mutual connexion.—The consistency of all the characters I have
enumerated with the theory of the organic origin of the Eozoic
limestone is no less remarkable than the difficulty of accounting for
their concurrence by any hypothetical combination of chemical and
physical agencies. It will be sufficient here to advert to a few
points of the case under this double aspect. If the relation of the
calcareous and siliceous components be such as is here maintained—
the siliceous residue left by decalcification being the internal cast of
the cavities, canals, and tubuli of the calcareous skeleton, and there-
fore being the model of the original body of the animal—every fea-
ture which it presents is found to be closely paralleled by the inter-
nal cast of a recent Nummuline shell. But if the collocation of
these two minerals has been the result of inorganic agencies, the
following points have to be separately accounted for:—1. The
succession of regularly alternating lamelle; 2. the segmental ag-
eregation uniformly presented by the siliceous lamelle; 3. the
occasional separation of the segments by calcareous septa; 4. the
structural union of both minerals in the proper wall of the chambers;
5. the peculiar dendritic formations carrying the siliceous component
into the very midst of the caleareous. Was the calcareous portion
first formed and the siliceous afterwards deposited by infiltration, or
was the siliceous portion first formed and subsequently penetrated
by calcareous deposit? if so, by what conceivable process of fissur-
ing could a system of cavities of such regularity and constancy of
arrangement have been produced? or if it be supposed that the
laming were successively superposed, what agency can be imagined
to have brought about the regular alternation of the materials? and
‘how can the segmental arrangement of both sides of the siliceous
lamine be accounted for? If each siliceous lamina were deposited
upon a preexisting calcareous lamina, its under side would take the
form of the subjacent surface: and how can the calcareous surface

altered by subsequent metamorphism,—a circumstance frequently met with in
rocks of undoubtedly organic origin. But in the numerous examples I have met
with of the arrangement referred to by Messrs. King and Rowney, it is so des-
titute of the characters of the true chambered structure and asbestiform layer,
that I should have no hesitation in regarding it as either originally a product
of inorganic agencies, or as the result of metamorphic changes in a structure
originally organic, which have caused the formation of the thick serpentinous-
layers in which these appearances present themselves.

1866. | CARPENTER—-EOZOON CANADENSE. 227

be supposed to have been hollowed out, so as to give to the siliceous
lamina exactly the same kind of tuberculation on its under surface,
as it is supposed on the mineral hypothesis to acquire on its wpper
by agencies inherent in itself? or if it be supposed that the calcare-
ous and siliceous salts were in solution in the same liquid, and that
the peculiar arrangement in question was due to their separation in
the act of solidification, the siliceous taking on the form of botryoidal
concretions, and the calcareous filling up the spaces between these,
the objectors may be challenged to bring forward any example of
an undoubted mineral produced by inorganic agencies which shows
anything like the structural regularity in the size and disposition of
its component parts that is presented by characteristic specimens of
the Canadian Hozoon*.

In addition to the localities in which it has been already announced
that the Eozoic characters have been detected in Serpentine Lime-
stone, I may record three as of special interest as indicating the
prevalence of the same features in that fundamental Gneissic for-
mation of Central Europe, which the labours of Sir Roderick Mur-
chison have shown to be the equivalent of the Canadian Laurentians.
Three months ago I received from Dr. Fritsch, of Prague, through
Mr. H. B. Brady, of Newcastle, a specimen of Ophicalcite from
Cesha Lipa in Bohemia, which gave on decalcification a form of
Eozoon closely resembling that exhibited by the “Irish Green.” Not
long afterwards I received from Dr. Hochstetter a specimen from the
fundamental gneissic rocks of the neighbourhood of Moldau, which
exhibited the same characters. And Sir Charles Lyell has recently
placed in my hands a specimen of Serpentinous Limestone sent him
by Dr. Gumbel, the Director of the Government Survey of Bavaria,
in which I have found what appears to me distinct evidence of Kozoic
structure, although it has.been greatly altered by subsequent meta-
morphism.

* This difficulty has not been met, so far as I can understand, by any of the
cases adduced as parallel by Messrs. King and Rowney. And it is further to
be observed, with regard to many of their arguments, that they are based rather
upon the appearances presented by the Serpentine Marbles of Connemara and
other localities which present the Eozoic structure in its least characteristic de-
velopment, than upon that of the Canadian specimens, which present it in its
least metamorphic condition. Every paleontologist who is acquainted with the
fact that even a recent Coral may be changed by atmospheric agencies into.
a crystalline limestone (see Sir C. Lyell’s ‘ Principles of Geology,’ 9th edit.,
p. 794), would feel the absurdity of maintaining that because the great mass of
the Carboniferous Limestone has now a crystalline or subcrystalline aggregation,
it cannot have been originally deposited as Coral in the manner indicated by the
structure of the parts in which the original characters of these ancient reefs are
best preserved. Yet this is precisely the line of argument taken by Profs. King
and Rowney in regard to the Eozoic limestones. It is the striking contrast be-
tween the features of the comparatively unchanged Hozoon of Petite Nation, in
Canada, and those of the obviously metamorphosed and perhaps disintegrated
Kozoon of Connemara, which most satisfactorily indicates the organic structure
of the former, by showing what mineralization has done, and therefore can do, in
the latter ; all this being in the contrary direction (if I may so express myself) to
the constructive action so obvious in the regular disposition of the component
parts of the former,

228 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

[ Note, June 29, 1866.—To the foregoing I may now add, that
having subsequently examined an extensive series of specimens of
Serpentinous Limestones from the ‘“ Fundamental Gneiss,” sent to
me by Dr. Gumbel, I find in some of them the precise parallel as to
Microscopic appearances with the most characteristic forms of the
Connemara Hozoon; whilst from these I can trace a continuous gra-
dation, through a series of phases which appear due to subsequent
metamorphism, to specimens whose characters seem purely mineral.
Appearances of precisely the same character are presented by a series
of specimens of the Serpentinous Limestones from the ‘‘ Primitive
Gneiss ” of Scandinavia, kindly transmitted to me by Prof. Lovén.—
In a communication I have received from Dr. Dawson, dated March
28th, he says :—-“ I have lately had my attention directed to a point
of importance noticed in my paper on Hozoon, but since somewhat
overlooked, the occurrence of Hozoon preserved simply in Carbonate of
Lime, without any Serpentine or other foreign mineral, and showing
the structure (that is of the canal-system, for I have not yet seen
the fine tubulation) as perfectly, though not so prettily in the matter
of colour, as the Serpentinous specimens. This fact alone, which
was noticed in my original Paper, and which I have now verified, is
of itself a conclusive answer to Professors King and Rowney’s objec-
tions.” ‘I may also say that a careful reexamination of the Chry-
sotile or fibrous Serpentine, with additional specimens, enables me
to reaffirm, if possible with still greater confidence, its entire distinct-
ness from any of the structures of the Canadian Hozoon.” |

January 24, 1866.

James Mason, Esq., F.C.S., Brighton; Wiliam Nevill, Esq., of
Langham Cottage, Godalming; and Henry T. L. von Uster, Ksq.,
3 Duke Street, Portland Place, W., were elected Fellows.

The following communication was read :—

On the Katnozorc Foraatrons of Brteium. By R. A. C. Gopwin-
Austen, Esq., F.R.S., For. Sec. G.S.

ConTENTS.

I. Introduction. 1, Physical Features.

II. Older Kainozoic or Crag Beds of 2. Zoological Features.
Antwerp. 3. Denudation.

1. General Remarks. 4, Variation in Depth.

2. Systeme Scaldésien. IV. Newer Kainozoic.

3. Systeme Diestien. 1. Cailloux Ardennais.

4. Schelle. . 2. Glacial Drift.

5. Louvain. 3. Campine Sands.

6. Berg. 4. Loss.

7. Bolderberg. 5. Polder Mud.

8. General Results. 6. Terrestrial surface.
III. Conditions of the Crag-sea area. 7. Sangatte Beach.

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIUS, 229

I. Inrropvucrion.

Tue following notes relating to the Kainozoic or Tertiary * formations
of Belgium were put together in the course of an interesting excursion
through that country in the spring of 1865, in company with Mr.
Hamilton, Mr. Prestwich, Captain D. Galton, Mr. W. W. Smyth,
Mr. Busk, and Mr. Gwyn Jeffreys. Our route was from Harwich to
Antwerp, Louvain, Hasselt, Maestricht, Liége (whence to Engis and
Engihoul), Namur. Some of the party went into Brussels to see the
collection in the Museum there; some to the Grotte de Han; in
company with M. van Beneden I had the advantage of seeing,
under the guidance of M. Malaise, the lower Paleozoic and fossi-
liferous rocks of Gembloux, which he considers to be of the age of
the Lower Silurian series of Sir. R. Murchison.

From Dinant, where we were joined by the late Mr. H. Christy,
we all visited, under the escort of MM. van Beneden, Dupont, and
other Belgian geologists and antiquaries, the caves of Furfooz on the
Lesse. An excursion in the neighbourhood of Mons, and a visit to
the coast at Sangatte, near Calais, completed the trip.

Some of our party had been in Belgium before, even repeatedly.
The points in its geology which on this occasion chiefly interested
us were the Crag-formation of Antwerp and elsewhere, the Boldérien
beds of M. Dumont, and the caves and recent researches at Furfooz.

To what extent the several members of our party may concur in
the views here recorded is a point on which I will not venture to
speculate; they are offered as my own exclusively; but I feel
bound to acknowledge the great advantage I derived from visiting
the district in company with so many experienced observers as
naturalists and geologists ; and we can all testify to the kind inte-
rest and assistance of the Belgian geologists, as also to that of the
military authorities at Antwerp, for which last we were indebted to
the exertions of Mr. J. Jones.

The cave-researches of Furfooz are under the superintendence of
MM. van Beneden and Dupont; for this reason it would not be
fitting that any comments should be made with respect to the views
which were freely communicated to us, until such time as the final
official report shall have been published. The question relating to
some portion of the in-filling is so closely connected with that very
complicated period to which the Loss, the Sables de Campine, and the
Cailloux Ardennais belong, that a few short references are necessary.

II. OtpEr Karnozotc orn Crac Bens or ANTWERP.

1. General Remarks.—By permission of the Belgian war depart-
ment, we were enabled to examine at leisure the deep sections
connected with the extensive military works in course of execution
around Antwerp; in addition we received the cordial assistance of
Captain Cocheteux and other Engineer officers.

‘The monograph of Mr. Searles Wood + had long since informed

* In this paper the author restricts the application of the terms Kainozoic and

Tertiary to deposits of the age of the Faluns and of more recent date.—Epir.
t Palxontographical Soc, 1848-1850,

230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

geologists how close an agreement existed between the marine fauna
of the Suffolk Crag and that of Antwerp. At the same time it was
evident from the work of M. Nyst * that there were many forms
met with in one area which were apparently wanting in the other,
and rendering it a matter of some interest in comparative geology
that such a difference within such narrow limits should be accounted
for ; this difficulty has long been a point of special interest in Ter-
tiary geology. The solution has been heretofore attempted by
various applications of the percentage test, as by the proportion of
recent forms to such as are unknown as living, or again by the pro-
portion which a given parcel of shells might contain, either of Arctic
or of more Southern forms. There has been so little agreement in
the results thus arrived at that some fresh solution should be
attempted. Percentage results, from their very nature, must ever
be fluctuating; the process when first proposed seemed specious, 1n-
asmuch as it had the appearance of possessing arithmetical accuracy,
but in reality it is the very reverse of this, in consequence of the
uncertainty of all the elements of the calculation and of their nega-
tive character.

M. Dumont proposed a twofold division for the Tertiary or Kaino-
zoic series of Antwerp, an upper or Scaldésien, a lower or Diestien.
Sir Charles Lyell’s account of the Antwerp Crag was prepared under
disadvantageous circumstances. At that time a few detached exca-
vations afforded the only attainable stratigraphical information, and
hence it became necessary to give the fossils collected at each loca-
lity in separate lists, thus producing the impression that the Crag-
formation there was both complicated and of considerable vertical
thickness, but such is not the case.

At the time of our visit an examination of the Antwerp beds was
extremely easy by means of two long artificial sections, one passing
along the main ditch of the new “ enceinte,” 14,000 metres in
length, the other along the ditch of the detached Forts, with a
length of 17,000 metres; thus giving 31,000 metres of continuous
section. These sections formed the subject of a short but very
useful memoir by M. Dejardin, Capt. de Génie, one of the officers
engaged on the worky. .

In the excellent Memoir by Sir Charles Lyellt, which has done so
much to make English geologists acquainted with the relations of
the various subdivisions of the Nummulitic and Tertiary formations
of Belgium to those of this country, the Tertiary series is arranged
as follows :—

§ 3, Antwerp Crag. 4
1. Yellow Crag = Upper Crag { Cello ion,

Steuvenberg, tab. 111 | gy stéme Sealdésien, Dum.

2. Crag gris—Middle Crag— tab. iv.

3. Crag noir—Lower Crag— tab. v.
§ 4. Sands and Iron Sandstone of Diest—“ Systeme Diestien” of Dwmont.
§ 5. Bolderberg Sands— “Systeme Boldérien,”

* Coquilles Tertiaires de la Belgique.
+ Bull. de l’Acad. R. des Sc. de Belgique, t. xiii. p. 470.
t Quart. Journ, Geol. Soe. vol. viii. p. 277, 1852.

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIES. 231

Of this arrangement it may be remarked that the “Crag noir” of
the local Antwerp geologists is distinguished from and made superior
to the Systeme Diestien of Dumont, whose S. Diestien at that place
(see Map, small edition) is described as consisting of “sable glau-
conifére coquillier” *.

M. Nyst’s latest subdivision of the Belgian Kainozoic series is as
follows :—

1. Yellow Sands, Steuvenberg, Calloo. Cyprina, Isocardia, Astarte.

2. Argillaceous Sands, Deurne. Cetacean bones, Pecten, Cyprina, As-
tarte.

3. Grey Sands. Pecten Gerardii, broken shells abun-
dant.

4. Grey running Sand. Bryozoa, shells scarce, same as J.

5. Black Sands, Edeghem, Berchem, Includes Pectunculus-band.

Ft, Herenthals.

In 1861 M. Nyst published a very interesting paper t, to which is
appended a list of 146 species of fossil shells and four Zoophytes ; of
- these, 58 had not been previously noticed as occurring in the Kaino-
zoic beds of Belgium.

The object of this paper is to state the result of that particular
enquiry which was of chief interest in connexion with the Antwerp
sections, namely the Zoological value of the subdivisions of the crag
beds there, and whether the proposed vertical order of arrangement
was correct in fact. Mr. Lankester visited Antwerp in 1864, and a
memoir communicated to this Societyt served to revive the interest
of these questions.

2. Systéme Scaldésien.—In order that the position of the Kaino-
zoic series about Antwerp may be understood, it must be borne in
mind that from the North Citadel on the Scheldt, as far as Deurne
(about half the extent of the “ enceinte”’), the level of the country is
below that of the river at high-water, which now rises 4:50 metres ;
low-water being 0°15 metre above that at Ostend. At this, the
north end of the section, where the Crag beds have been laid bare
beneath polder mud, its upper surface is at about low-water level,
and at nearly the same level are the beds so rich in shells, out of
‘which the Docks have been excavated, from beneath peaty beds and
polder mud. We collected largely from these shell-beds, or rather
from the spoil-banks. The assemblage is that given by Sir Charles
‘Lyell, tab. i1. and iii., and by M. Nyst, list 34, p. 6018.

North of Deurne the glacis has been formed out of the spoil from
the main ditch, and shows that it has been excavated out of an ex-
tension of the same mass of sands, gravel, and broken shells, as
above. South of Deurne the ground rises somewhat, and as the
works were then in progress, good sections were to be seen from 4

* Tabl. des Terr. &c. de la Belgique.
__ t Notice sur un nouveau gite de fossiles, se rapportant aux espéces faluniennes
du Midi de l'Europe, découvert 4 Edeghem prés d’Anvers. Bull de I’Acad. R.
des Sc. de Belg. t. xiii. p. 29. See also Lyell’s ‘Elements,’ 6th edit. p. 232.
~ $ Quart. Journ. Geol. Soe. vol. xxi. p. 221, 1865.

§ Omalius, Abrégé de Géologie, 7¢ édit. 1862.

232 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Jan. 24,

to 6 metres deep. The blocks left for measuring the work done
show such sections as the following :—

Yellow sands, gravel and broken shells.
a. Systeme Scaldésien... + Grey sands, numerous broken shells.
Brown sands.

Pale-green sands, shells few, not much broken.
6. Systeme Diestien...... Dark-green sands, Pectunculus-band.
’ | Very dark compact beds,

The relative thicknesses vary much from place to place; the whole
not being more than 12 feet thick, of which the upper brown and
yellow sands form about 6 feet. In the Dock-sections these upper
beds may have been somewhat thicker, but at no place do they pro-
bably exceed 8 feet.

The upper series (a) constituting the ‘‘ Systéme Scaldésien” of
M. Dumont, viewed as a marine accumulation, presents a very com-
mon condition of sea-bed, consisting of dead-shell gravel, mostly
forming banks, and heaped up under inconsiderable depths of water.
This is a good division of the series, inasmuch as it marks a change
in the depth and moving power of the water at this particular spot,
the result, doubtless, of a physical change of wider extent; the
effect. of which was the disturbance of previously formed sea-beds
and their rearrangement. At the same time there was an outward
distribution of the materials of a higher or sublittoral zone, as seen
in the gravel.

The “ Systéme Scaldésien,” as exhibited at Antwerp in tie form
of “ couches remaniés,” very closely resembles both in the condition
of its materials and fossils, the Red Crag beds of Suffolk; nor is
there any reason why the physical change which caused the
Red Crag to succeed the Bryozoan should not be referred to the
same geological change which made the Scaldésien follow on the
Diestien. Aen:

3. Systeme Diestien.—In the section given above, which is just
such as is to be seen everywhere from the Porte de Tournhout to
that of Malines, the Scaldésien beds, or yellow and grey coarse series,
contain either fine pale-green, somewhat loose sands, or else dark-
green, almost black, and compact sands ; these are the Diestien beds
of Dumont. With reference to condition of sea-bed, it-is that form
well known as deep-water sandy and muddy ooze, and was the de-
posit of tranquil depths.

Although the whole thickness of this lower series has not been
cut through within the area of the fortifications, even in the section
above referred to, which presents the deepest cuttings, yet it has
been proved, as we were informed by the Engineer officers on the
spot, that the Diestien beds extended only a few feet below the
excavations for the main ditch, and that within the area as well as
without, the dark-green Diestien beds overlie compact Rupellien
clay.
A maximum thickness of about 4 metres may be assigned to the
Diestien beds; generally they are less, and small as are the vertical

1866. ] GODWIN-AUSTEN—BELGIAN TERTIARIES. 233

dimensions of the whole of the Crag series at Antwerp; there is no
other place in Belgium where they are so thick—indeed, beds of the
true Scaldésien, Crag-like type, occur only at that place: it is also
the only spot where fossiliferous Diestien beds have been observed.

The Diestien beds of Antwerp represent a condition of sea-bed
over which submarine life is abundantly developed, and that with a
distinctive facies. Viewed in this way the sections from the Porte
de Tournhout are exceedingly interesting, presenting a rich and
varied fauna, of which a full enumeration has recently been given
by M. Nyst (Bull. de Acad. Roy. des Sciences de Belg. 1861, sér. 2.
t. xu. p. 20). One particular form, the Pectunculus glycimeris,
numerically exceeds all others by 1000 to 1; it colonized this area
of the Crag sea, attaining a large size, and forming banks which in
places are not less than 24 feet in thickness. The Diestien was a
true life-zone, and exceedingly prolific, and as such it is in striking
contrast to the Scaldésien division, of which the whole of the as-
signed fauna is from dead and drifted shells: it may safely be
asserted that of the shells met with in the Scaldésien beds not one
lived where it is now found; this, from a natural-history point of
view, is the real difference between the upper and lower Crag of
Antwerp. |

The area over which the Scaldésien shell-gravel and the fossili-
ferous Diestien ooze are to be seen together is even now so limited
that much generalization would be hazardous. Traced from below
upwards, the Antwerp sections show a gradual passage from very
fine and dark muddy ooze into sandy ooze, and finally into fine pale-
green clean sand; in this there is a clear indication of a slight in-
crease in the moving power of the water: a slightly diminishing
depth might cause such a change. The more sandy beds, where
they remain, form the uppermost portion of the Diestien division,
and contain but few shells.

The Scaldésien division overlies an eroded surface of the Diestien,
and is found on every component portion of the series down to the
lowest and most compact beds. ‘The line of separation is always to
be traced, and is mostly very distinct—it marks a sudden change of
condition ;—but as in the Diestien so in the Scaldésien series, the re-
arranged pale-green sands, brown sands with shells whole or broken,
the dead-shell hanks, and uppermost the thickest layer of gravel with
pounded shells, indicate a progressive change and slow shallowing.

The bathymetrical conditions indicated by the Scaldésien and
Diestien accumulations may be judged of by the guidance of the
soundings over the English channel; the difference may have been
as much as from 30 to 40 fathoms, or to such an extent must the
crag -sea have shallowed about Antwerp from the time of the shell-
bearing Diestien beds, their denudation, and the formation of the
dead-shell sand and gravel bank. The Pectunculus glycimeris, the
most abundant member of the fauna, ranges from 25 to 60, and,
according to some, to 100 fathoms; but no part of the Diestien beds
indicate a depth at which Dentalia become abundant and charac-
teristic, such as 80 to 100 fathoms. }

VOL. XXII.—PART I. : S

234 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 24,

I received from Captain Cocheteux, a small but very interesting
collection of fossils from the lowest Diestien beds in the neighbour-
hood of Fort 4, towards Edeghem (see list) ; but we did not visit the
Edeghem brickfield-section above referred to as described by M.
Nyst. From. recollection of what I saw in 1861, the Diestien beds
exactly corresponded in colour and composition with those of the
enceinte. The only place near Antwerp at which we saw the super-
position of the Diestien Crag to the Rupellien clay was at Schelle.

4, Schelle-—The Crag-sea accumulations of the several localities
to be noticed have been called Diestien, but they belong to very dif-
ferent submarine conditions from those of the base of the Antwerp
Crag. |

As at Edeghem, beds of Rupellien clay are worked extensively
for bricks and tiles at Schelle. This Rupellien clay is an upper
member of the Nummulitic series of Belgium, corresponding in age
and condition with, and externally very like, our Barton clay of Hants.

The Rupellien clay is capped by sandy beds, which, towards
their base, and particularly at the upper end of the section, become
as dark as those about Antwerp, though they are not so thick.
These sands are altogether about 3°5 metres thick. A very dis-
tinctly marked line separates these formations; at one place there _
is unconformity on an eroded surface, and throughout there is a line
or band of flints, some large, remaining in place, together with Sep-
tarie from the Rupellien clay; one of these measured more than
a foot across. These Crag beds belong for the most part to the drift-
sand sea zone. ;

At Schelle the upper surface of the Crag sand has been eroded,
and at either end of the section the denudation has been carried
down to the Rupellien clay. Schelle is 10 kilometres south of
Antwerp, and the great interest of the section, as of that of Edeg-
hem, consists in the evidence it affords of the complete break of
continuity between the Rupellien clay beds and the overlying
Crag.

5. Louvain.—Louvain is between 4 and 5 myriamétres south-east
of Antwerp. The remains of the Crag-sea beds occur only over the
Belgian area in detached patches, and the interest of this locality
consists in the evidence it affords of the great depth to which denu-
dation of a date subsequent to the Crag period has been carried.

We were conducted to an interesting section on the side of a line
of hill, on the road from Louvain to Pellenberg;,and Tirlemont, by
M. Van Beneden, who had with him a diagram prepared by M. Du-
mont. The upper part of this section alone is referable to the Crag,
the details are given in fig. 1.

On an eroded surface of white and yellow marls, the equivalents
of the Rupellien clays, according to Dumont, is first a line of chalk-
flint shingle and gravel, surmounted by brown and ferruginous Die-
stien sands; these beds belong in a marked manner to the sea-
zone of drifting sand. The uppermost portion of this capping to the
hill consists of ferruginous sands distinctly bedded, occasionally dia-
gonally, and below this is a line of waterworn flints on a scored sur-

1866. } GODWIN-AUSTEN—BELGIAN TERTIARIES. 235

face. The upper series is somewhat coarser than the lower, and
indicates a local change, or disturbance of sea-bed; the whole of
the crag accumulation at this place is sublittoral.

Along the valley of the Dyle denudation has removed all beds
from the Crag down to the Bruxellien of Dumont, or Lower Num-
mulitic.

Fig.°1.—Section showing Crag-sand and Shingle capping a hill east
of Louvain.

SS ——__—— ———— = 2

+ 2,0 Mee O6 SF.
a
MO Th MEM I ut / TO (tll. 3

1. Flint shingle.

2. Very ferruginous sands, with flint shingle at the base.

3. White and yellow marl (Argile de Boom) underlain by Lower
Rupellien sands.

6. Berg.—The furthest point to the E.S.E. of Antwerp, distant 7
myriamétres, at which we saw the rolled flints and yellow sands of
the Crag-sea area, was at Berg; these gravel beds were pointed out
to us as belonging to the base of the Campine sands, but the circum-
stance that the gravel is wholly composed of chalk flints is against
such a supposition. These Crag beds, which indicate littoral condi-
tions, overlie the uppermost portion of the Nummulitic series (Ton-

_ grien).

7. Bolderberg.—Our visit to this place was the most interesting
point of the excursion: the locality had suggested to M. Dumont
his “‘Systéme Boldérien;” as such it was adopted by Sir Charles
Lyell (ube supra, tab. 1. p. 270) as also by MM. d’Orbigny* and
Beyricht. The Boldérien formation or division has therefore a two-
fold interest :—I1st, in respect of its distinctiveness or place as a
marine sedimentary group, 2nd, as to its zoological value.

The section of the Bolderberg is well given by Sir Charles Lyell
(u. s. p. 295), except that the position of the shingle-bed on an
eroded uneven surface of the subjacent sandy strata is not repre-
sented in the woodcut. To whatever period the lower sands may
belong, it is evident that they had become consolidated before the
accumulation of the shingle. The shingle is wholly made up of -
chalk- flints, in which respect it agrees with the lines of gravel and
shingle in the Louvain section (fig. 1), and also with that at
Berg.

M. Dumont’s systematic subdivisions were based on considerations
of composition or mineral character; and in accordance with an
assumed theory of geological change he considered that shingle-beds
represented a break or division in a series of accumulations, and
further, that the shingle- or gravel-beds were referable to the close

* Cours Elémentaire de Paléontologie, t. ii. p. 765.
+ Ueber den Zusammenhang der Rotdioatachen Tertiarbildungen, ibuendl:
der k. Akad. der Wissensch. zu Berlin, Aus dem Jahre 1855, pp. 1 e7 seq.
s 2

236 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 24,

of a geological period. In the case of the Bolderberg there was no
difficulty in identifying the upper ferruginous sands with those of
Diest, and overlying some older system, endimg upwards in a shingle-
bed.

So far as the “‘ Systeme Boldérien” of M. Dumont is concerned,
its geological value is dependent on this simple consideration,—Is the
shingle-band connected with the sands below or the sands above?
In nine cases out of 10 throughout the whole series of geological
formations the shingle, gravel, and conglomerate beds form the base
of each natural group of accumulations. In the case of the Bolder-
berg there is no ambiguity whatever, the break and unconformity,
whatever it may be worth, occurs below, and from this line there is
a progressive change upwards from sands with shingle to sands
without ; the whole mass of the upper ferruginous sands forming a
continuous series, and differing from the capping to the hills about
Louvain only in the circumstance of the fossils it contains. The
lowest bed represents a littoral line; the higher sandy beds, the
zone of drift-sand and of the Crag sea; the whole haying been ac-
cumulated slowly as the area was being depressed or submerged.

Zoologically, the “Systeme Boldérien ” has been represented as a
true Miocene formation of the age of the Faluns of Touraine*, and
this has constituted its paleontological interest. Sir Charles Lyell,
with the assistance of MM. Nyst and Bosquet, gave a list of 47
species of fossil shells which presented this difficulty—that whereas
the Faluns of Touraine do not contain a single form belonging to
the Nummulitic formations, even those of its latest stage, but have
a marine fauna, which so far as accurate identification has gone, is
wholly Eastern Atlantic, the reputed Boldérien Miocene fauna has
had assigned to it a mixed assemblage of North-Sea Crag shells,
(recent species), and those of the Belgian equivalents of our Barton
beds. It was this consideration probably which caused M. d’Orbigny
to refer it to his “ Sous-étage Tongrien” }; indeed, it is evident
that it was the Bolderberg list which produced this double error.

We collected a considerable number of the fossils of this locality.
They occurred, as stated by Sir Charles Lyell, in the pebble-beds
and associated sands, they are for the most part broken and worn,
and “ resemble shells thrown on a sea-beach” (wu. s. p. 296). The
_ great preponderance of single valves and of fragments of Pectunculus
glycmeris, and Crag forms of Pecten, Venus, &e., gives to the assem-
blage the aspect of the Scaldésien fauna ; but with these are Diestien
forms of Lunulites, Flabellum, and the little Ohva flammulata, all
exceedingly well preserved. Even at first glance the fauna of the
Bolderberg sands is to a very great extent identical with that of the
Belgian Crag.

Sir Charles Lyell’s list, when cleared of all species respecting
which doubts were felt, leaves 23 forms. M. Nyst’s more recent list
also contains 47 species, but differing from the 47 given by Sir C.
Lyell. Taking the first list, some of the identifications were erro-

* Quart. Journ. Geol. Soc. vol. viii. p. 279.
t+ Cours Hlém. de Paléont. &c. t. 11. p. 764.

1866. ]. GODWIN-AUSTEN—BELGIAN TERTIARIES. 237

neous—Corbula pisum, Cancellaria evulsa, &c., have been recognized
as such—some, it will be seen, are as yet peculiar, others have been
described from imperfect or single specimens ; eliminating these, the
remainder are true Crag-shells and also recent species, so that the
list no longer presents the admixture of Nummulitic and recent
species as was once supposed.

The Boldérien fauna was considered to indicate a warmer climate
than that of the Antwerp Crag (wu. s. p. 297); but since the pub-
lication of Sir Charles Lyell’s Memoir, the “Crag Noir,” or “ Systeme
Diestien ” has afforded all the forms of Oliva, Conus, Ancillaria,
and Cancellaria, from which such conditions were inferred.

The Bolderberg is the only locality where the evidenee of a Bol-
dérien system, stage, or subdivision has been met with in Belgium.
Of the newer formations of the Rhine valley, those of Grafenberg
near Dusseldorf can alone, says Beyrich, be placed on the level of
those of the Bolderberg ; but he adds that it is very doubtful whether
these do not rather belong to the older Sternberg beds or Tongrien ;
so that, both on purely geological as on zoological considerations, the
Boldérien system may be removed from the general series of distinc-
tive geological groups.

Since the above was written, I have met with the following pas-
sage by M. Nyst—the result of a comparison of the Edeghem shells
with those of the Bolderberg :—‘‘ Ce qui nous fait penser que le
systeme Boldérien n’est que la base du systéme Diestien de Dumont.”
It is true that the Bolderberg shells agree with those of Edeghem
and Fort Herenthals; but inasmuch as the Bolderberg shells have
been washed out of older beds, the Systéme Boldérien, as an accumu-
lation, must necessarily be of later date in the Crag series, and not
its base or oldest portion.

8. General Results—The study of the Antwerp sections leads to
the impression that the vertical dimensions of the whole of the Crag
formation there are exceedingly small. From the highest ground
(ligne culminante) down to the sea-level, the depth is only 9 metres,
and within this is comprised the whole formation, including the
Campine sands. As it happens in Suffolk*, so here, where the
upper or Scaldésien Crag is thickest, the lower is thinnest; and
where the Diestien is thickest, the upper is thinnest, or at times
wholly wanting. If the Diestien beds be divided into upper sandy
ooze and lower muddy ooze, the sections show that where the first
has been removed and “‘ remanié,”’ the resulting Scaldésien beds take
the form of “ Crag gris;’’ and that where it has not, there are then
yellowish, argillaceous, and gravelly sands. The real difference be-
tween. the “Crag gris” and the “ Crag jaune” of the Belgian geo-
logists is, that the first contains a larger proportion of the ‘“re-
manié fauna” of the Diestien beds; and although they may, as
already stated, have been produced under slightly differing condi-
tions, and in sequence, yet in the horizontal sections they replace one
another, and have not an aggregate thickness of 4 metres. If, as

* In the Deben valley the Crag does not exceed 25 feet, and even in the Ips-
wich district it is of small amount.

-238 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

was most probably the case, the Scaldésien accumulation was of the
nature of a dead-shell sand and gravel-bank, like the “ cordons litto-
raux ” of the English Channel and North Sea, and so merely a local
condition of sea-bed, the estimate for the thickness of the Crag must
be still further reduced: the ordinary minute subdivisions of syste-
matizing geologists are wholly inapplicable to such accumulations
as these.

From this it is evident that the Antwerp sections fully satisfy the
inquiry as to relativeage. The Scaldésien division there is younger
than the Diestien, as it has been accumulated over it. So likewise
the upper Scaldésien must be younger than the lower; but this is
merely relative age in respect of rearrangement. The corresponding
conditions on the English and Belgian areas of the Crag sea are the
Red Crag and the Scaldésien ; both are “ remanié” accumulations.
The difference which these present in respect of the marine fauna
they contain, is not of much amount numerically, and, viewed in detail,
it is just such as would arise from the different sources whence each
was derived. The Red Crag was from the break up of a neighbour-
ing Bryozoan sea-zone, the Scaldésien from Ooze depths. Any com-
parison of the fossil contents of the “ Coralline Crag” and of the
“Crag noir’? must be subject to the consideration of differences
which result from depth and condition of sea-bed. From the nature
of the question, therefore, a percentage calculation for determining
relative age is inapplicable with respect to the component parts of
the English and Belgian Crag, or even of one part with another of
the same series.

The fossils of the Systéme Diestien are proper to it; and from
them may be inferred the condition of that part of the Crag sea for
that particular time. The fossils of the Scaldésien beds are wholly
extraneous to them, belonging to all regions of depth, and all
periods of the Crag formation—from them no guidance in geological
chronology can be derived.

III. Conprrrons or Crag-Sea ARBA.

By combining the results obtainable from the East Anglian and
Belgian Crag beds, some general views may be deduced as to the
Crag sea, both physical (1) and zoological (2).

1. Physical Features.—Along the lower courses of the Orwell and
Deben, and thence towards Orford and Aldborough, the Crag beds
occupy an old depression. The greatest extension which the sea
had here was by Bentley, Ipswich, and Woodbridge. The Red Crag
of these places being a true sub-littoral accumulation.

Corresponding beds, as to age, occur in two other old depressions,
those of the Blyth and the Yare. At Yarmouth it may be inferred
that there is a considerable thickness of Crag (Prestwich, Quart.
Journ. Geol. Soc. vol. xvi. p. 449). Finally, a sea-bed of the same -
age is seen at Mundesley. In tracing the outline of the Crag sea, it
may safely be made to include a rather wide area, about the lower
courses of the Waveney, Yare, and Bure.

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIES. 239

Rivers discharged at several places, bringing down the land and
freshwater shells of the period into the Crag sea, of which forms the
Unio litoralis and Cyrena consobrina are the best guides. On one
side of this sea, the Grays beds represent the purely fluviatile or
estuarine beds of the great tributary of the Thames valley ; whilst the
Norwich beds and those of Kelsey belong to the fluvio-marine facies,
in connection with the streams or rivers of the Yare and Humber.

North of the East Anglian area the Crag sea is indicated at inter-
vals, as at Bridlington and Stains (Aberdeenshire), and by its fossils
over the bed of the North Sea.

In addition to the conditions here given, we have on the English
side of the area the Coralline Crag, or Bryozoan facies of its sea-bed.
_ From near Maastricht the Crag beds extend beneath newer accu-
mulations into Guelderland (Winterswyk, Rekken)*.

The shelly sands which in North Holland occur beneath the Dune-
sand, Polder-, and Peaty-beds, are, undoubtedly, of the Crag Period,
and the same sea-bed is met with in Segeberg, Liineberg, and Sylt ;
but it does not extend eastwards into the Baltic area, and that
depression owes its origin to a subsidence or depression of the great
Scandinavian mass, the line of which, very probably, is that of the
deep-sea soundings, and which accordingly has been taken (wide
Map, fig. 2).

The Crag sea opened out northwards. On the extreme south its
condition is indicated, first, by the great breadth of the sand-zone,
extending the whole length of the axis of Artois, and the Ardennes
chain; and next by the transport, along a line of coast, of the
flint-gravel and shingle, which must necessarily have been derived
from the English side of the area. As these materials occur from
the basement bed to the uppermost, such a coast-line must have
been continued during the whole of the Crag-sea period, as a limit
on the South. Structurally, the limitation was dependent on the
extension of the axis of Artois, and of our own Wealden elevation.
The Sangatte section shows that this barrier was maintained until
the close of the Glacial Period*.

At this time the Northern hemisphere presented a broad belt of
circumpolar land, and these geographical arrangements influenced
the character of the Crag-sea fauna.

Such a communication as the present does not admit of a detailed
analysis of the Crag-sea fauna in respect of its origin, though the
. materials are amply sufficient, but the subject may be alluded to,
inasmuch as the peculiarities can alone be explained by reference to
bygone geographical arrangements.

What these must have been is given in the accompanying small
sketch-map, which shows why the Crag Molluscan fauna, which is
wholly Atlantic, like that of the synchronous sea-beds of Selsey, the
Cotentin, the Faluns of Touraine and Bordeaux, &c., should differ
from these last to so great an extent. The Crag-sea area included
the representatives of two distinct Atlantic provinces, the Boreal or

* Staring. Bodem van Nederland. vol. ii. p. 284.
T See pat Hist. of European Seas, p. 286, and Map IT.

|e
| en ead =
i if 4)
, i

t Z \
= J | Ht ? ? oe aN
= sell i vi 7 we XM
> | TiS We a as
Ey ce
a Ee
A Ne Ye ce
AW L e Z
| = S i 2G Bee
| | i SK Nee Ee
SS SS eS ot
—, = ix an Bee
A (= Ste S 2
=
= te :
HA. lite fee
yuh Baa
il Sl =~ ia _- SS
Z G cal ~ as
OKA -@ SS
ait 7 Yi SS
a Ny Y SS
Deed
ter NOH
fp NG,
Fe ESM f
Uo RS
wee VA ‘~~
2 ¢ /
7 y uh
= // /
Yj S I
Y, Gj |
Yi,
GY, J I}

ROS vans
YS
7
Y i,

int indicates ancient la

tint indicates ancient seas.

int indi present land that has not been sub-
merged during the Crag period.

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIES. 241

North Atlantic, both Eastern and Western, and the Southern or
Lusitanian.

The greater extent of cireumpolar land would exercise a great
influence on the course of the North Atlantic Ocean-current, and the
general temperature of its waters,from 55° to 65° N. lat., would have
been much higher than at present. Under these conditions there
would have been an extension eastward of the transatlantic littoral
fauna, whilst at the same time the temperature would encourage a
more northern range of Lusitanian forms.

The marine beds of the Tagus, of the Adour, of the Loire, and of
the English Channel, which were indents from the Eastern Atlantic,
have this common characteristic, that the fauna of each, so far as
living species can guide us, is more southern than that of the corre-
sponding coast at present ; and this order of difference is progressive
from south northwards, so that whilst the beds of the English Channel
have Lusitanian relations, those of Touraine, and to a greater extent
those of Bordeaux* and the places south connect themselves with the
West African marine fauna.

2. Zoological Features.—The Crag fauna of die English area is in-
complete, so also is that of Béleviin « taken together, they form a
completer marine fauna, representing a greater range of sea-zones.

Various comparisons have been made for percentage calculations
between the shells of the “ Crag jaune” and the “Crag gris,” and
again between those from the Scaldésien generally and the “ Crag
noir” or Diestien.

It will not be necessary here to reproduce the whole of M. Nyst’s
latest lists, given in the work of Omalius; for the first comparison
the differences in the first two lists will suffice. It might be ex-
pected, from the extent to which the Diestien beds have been denuded,
that the whole of their proper fauna should be met with in the
Scaldésien beds which resulted from that change ; it is so to a great
extent, but it is also evident on the spot that it is mainly the stronger
shells which have endured removal; besides this, in the Antwerp
district, where alone true Scaldésien beds occur, the Diestien beds on
which they lie have not been denuded quite so low as the second
life-zone (Edeghem, Fort Herenthal), in which the deepest water
assemblage is met with.

It would appear, so far as collections at present indicate, that of
143 species enumerated by M. Nyst, there are some in the “ Crag
jaune ’ ’ which are scarce or wanting in the “ Crag gris” (Tab. I.),
and in the latter, some wanting in the other (Tab. II.) ; but the lists
may be somewhat reduced by removing such species as are known
only as Belgic at present. Paludestrina? terebellata, N.; Turbinella
imternodula, N.; Eulima levis, N.; Natica proxima (a doubtful
species); Cancellarra minuta, N. (an seul individu); Pleurotome
turrifera? P. costata; P.histrix ; P. Woodii; Murex tortuosus, M. C.

* The boundary of the Crag sea is so traced on its eastern side as to include
the Upper Kainozoic formations near Cassel, Luithorst, Freden, and Dichholtz ;
these are all in the latitude of the Belgian crag, and along the courses of the
Weser and Lesse.

242 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

(a deformity of M. erinaceus); Trophon striatum; Cerithium Wood-
wardi, N.; leaving for Tab. I. 16 peculiar species.

Taste I,

( The species with an asterisk occur in the Edeghem zone.)

Rissoa. i
vitrea, Mont. .......... ren ae in ie le SJE | Bryozoan Crag.
TURBO.
*plicata, Mont. ............ Pier dbase ee Bry. Cr. Subap.
- Acton.
*Nox, M.C.=A.tornatilis Borealand Lusit.40faths. Bry. Cr.
ToRNATELLA.
conoidea, Bre. =T, plicata, |
Mont.; fide Alder,
1S TLE ARE FR A AEA OE i
Natica.
Sowerbyi, V.=catenoides { Boreal and Lusit., litt.,
= nitidy Ae ee. { A0fithe ve een } Rem Cr
TrRocuvs.
papillosus, Da C.=similis, he Brit. to Lusit. litt.,) Red Cr. 7. simélis in
IM eT ioc are Slenls voeastsge see 50 faths. ........2..-.+-++- “ Crag gris.”
CINETATIUS Li. o.ccseceson one eens Brit. litt., | Red Cr.
CANCELLARIA.
costellifera, J. C.=viri- { Greenland Eur. Boreal,
dulak pineal Seas { HOURS HNS, 0 Je cecsee By ee
umbilicaris, Bre.=cancel- { Lusit., W. African, 4-25
lata=similaris ......... PAGS ucsena ee «psesemionaee
PLEUROTOMA.
*turricula, Bre. non Bela- Red Cr. It. Sic. (Bol-
p tur. SE REM AL, Si. acbie gall le ghee earl an aero eel ena hue area derberg).
elegans, Scac.=attenua- {N. Lusit. to Mediter- | Touraine(Pl.incrassata,
(SU eel .(07 (7 cas sm ranean, 6-25 faths....... De}.).
PLACUIS, SCAN. Me che deeey Brit. to Lusit., 8-30 faths.
TROPHON.

scalariforme, Gould=cla- { Boreal and Brit. litt. to Red Ge
thratum, L. fide Lovén. HOO tats: reese ;
tetragona, M. C.=capil- ae to N. Lusit., a Red Cr. (a deformed

AUS HG. 0. aaah ees FaLWS re. ice variety).
CrERITHIUM.
punctatum,. Wood. vic: .s...se0tencccvne accngesscccnoesese sede. ved Cr, Touessulaam:
Nassa.
prismatica, Bre........0.....0- Lusit., 20-40 faths. ...... ee E aa Red Cr. Tour.
ubap.
Buccinum. |
crassum, NV.=Dalei, M. C. Borealand Lusit., 8lfaths. Red Cr.
PATELLA. tee
virginea, Mill. ve... aerate Tacit i aa Red Crag.

1866. ] GODWIN-AUSTEN—BELGIAN TERTIARIES. 243

In like manner the following may be deducted from the list of
“Crag gris” shells :—Scalaria Woodiana, N.; Turbinella somilis ;
Cerithium simstrorsum ; Nassa flexuosa ; N. crassilabra; N. contorta ;
Pileopsis militaris, Mont. (a spurious West-India shell, F. and H. iu.
p. 462) ; Dentaliwm semiclausum ; leaving 16 peculiar species, viz. :—

Taste IT.
PYRAMIDELLA.
: Bry. Cr. Tourain. fal.
EMBs o ke coat ign cuisinchecien ed s oh bsudaeoeneone { jaune, Bord.
SCALARIA. ’ ;
clathratula «............0000 ie Sen ee OER. } Bry. Cr.
AcTxon.
*levidensis, Sw.=tornati- { Brit. to Spain, litt. to 40] Bry. and Red Cr. (in
lis, L.=Nox, M.C. ... PaptNAy ck oie hid ban Bek J tab. i.).
RinGicuna.
*buccinea, M. C.=auricu- 4 Bry. and Red Cr. Bord.
BA Mond oo... \ Se { Subap.
TROCHUS.
similis, M. C.=papillosus W. Brit. to Canaries.. ... also in tab. i.
Sele oi aaneeer omer Bry. and Red Cr.
102A el

conulus, Z.=zizyphinus, ) 7... 1:
southern fone oft | Lusit, itt. to 40 faths. ... Bry. Cr.

ManrearirTa.
ee Bry. Cr
PLEUROTOMA.
y : Red Cr. Dax. Subap.
UMMM RS eee oc acu dere nsdmasaceecwengeawence§ (Steuvenberg).
TROPHON.
alveolatum, MC. ....1..12 seseseccsecsenenerengeerterentees Bry. Or. com. Red Cr.
aribiquam, W105... .cc...e. { ae to W. Lusit. and Cr. passim.
muricatum, Mont. ......... aii eon mele Bry. and Red Cr.
PyrvuLa.
Peetain. Lan ee and Red Cr. Tour.
Iy z= @ereeeeee *§ Ceesereen @eOSCeceeseoreceseseseseeseeen Subap.
Nassa.
* lata, MM. C., var. of { Boreal and Lusit. litt. t
granulata, , var. O (a)
ECTASSALA «22.22.0020 s000. { 50 faths. | Bry, and.Hed Cx.
CASSIDARIA.
Scena Uxternige
ae ey ey \ busit. 6 faths,.c4.. 00.26. Bry. and Red Cr., rare.
PILEOPsIs.
obliquus, Sw.=ungaricus, ) Brit. and Lusit. 15-30
Val op cme aes cteblAies TACIISA eeisinnccaede A et ae
DENTALIUM.

costatum =dentale, Lin... Lusit. 2-30 faths. ......... Bry. and Red. Cr.

244 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 24,

The Conchifera from the “ Crag jaune” and “ Crag gris” are the
same ; the differences are solely in respect of the gasteropods. The
distribution in depth of the living analogues of the Crag conchifers
will satisfactorily explain this; and the only other inferences which
these tables suggest are, Ist, that the species generally indicate a
greater depth of water, as their life-zone, than that of remanié Scal-
désien beds in which they occur; and, 2nd, that these deeper
zones of the Crag-sea had very decided southern or Lusitanian
relations.

M. Nyst is of opinion that the marine fauna of the lower Diestien
beds (Crag noir) is more nearly allied to that of the Faluns of
Bordeaux, Piedmont, Sicily, and Austria, than that of the Scaldésien
Crag. This view is hardly supported by a consideration of the 25
species of Conchifera which occur in the Edeghem and Fort Herenthal
zone. As the product of the shallower-water sea-zones which con-
tributed the Scaldésien fauna, shows decided southern relations, the
deeper-water zones would necessarily show a like relation somewhat
more strongly, from the more uniform conditions which obtain there.
This is just what happens now. This impression as to the Falunien
facies of the lower Crag is very likely to suggest itself, from the pre-
sence of corals such as Stephanophylha, Flabellum, and the marked
preponderance of such genera as Cancellaria, Fusus, Plewrotoma,
Conus, many of which are so very like Barton and Rupellien species
as to give an even older aspect to these beds. All the Diestien spe-
cies are, however, distinct, and these resemblances are good illustra-
tions of that system of representation which is to be observed in
respect of the products of like conditions and zones of depth of every
geological period.

M. Nyst’s list of Edeghem shells may be reduced from 145 to
130 in respect of uncertainties; of these 47 are known as living.
This gives a seemingly larger proportion of unknown to known
forms than is the case with the Scaldésien Crag. The question which
arises is, whether this difference 1s connected with relative age,—
whether it is any proof that the Edeghem beds are of greater anti-
quity than the Scaldésien. Geologists have so considered it.

The 47 species above referred to are as follows,—L. signifying
Lusitanian province, Br. British, B. Boreal.

TaszE IIT.
Chemnitzia similis, Forbes. L. Mitra fusiformis, Broc. L.
Pyramidella plicosa, Bronn. L. Aporrhais pes-pelecani, Zin. B.-L.,
Odostomia plicata, Broc. B.& 8. L. 100 f.
10-70 f.. Pleurotoma intorta, Broce.
Actzeon tornatilis, Zin. B—L., 3-60f. | Nassa incrassata, Miid/. B.-L, litt.—
Ringicula buccinea. L., 4-60 f. 50 f.

Natica millepunctata, Lin. L. litt40f. | Cassis Saburon. L.-W. Africa, 8— ?.
Josephinea=Olla. L., 8-12 f. Calyptreea sinensis, Zin. S. Br.-L.,

Cyprea pyrum, Gm. L., uncertain. _ htt.-1lof
Europza, Mont. B. & L., litt— | Crepidula unguiformis. L.
20 f | Emarginula fissura, Lin.

Oliva flammulata. West Afr. Dentalium entalis, Lin. L,, 2-200f.

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIES. 245

Taste III. (contenued).

Bulla lignaria, Zin. B.-L., litt.—40f. | Venus rudis, Poli. L.
cylindracea, Brug. B.-S.L., litt. | Venus chione, Lin, 8. Br. & L., litt.

-90. 40 f.
acuminata, Brug. Corbula gibba, Ov. B.-L., 5-30 f.
—— conuloidea, Wood. Cyprina Islandica. B. & Br., 5-80 f.
utricula, Broc. Mya ferruginosa. N. Br., L., 3-80 f.

Vaginella depressa. Lusit. latitudes. | Axinus sinuosus. B.—L., 8-80 f.
Spirialis rostralis. ‘othe Lucina borealis. B.-L., litt.—80 f.
Pholas papyracea. S. Br., litt.—20 f. Pectunculus glycimeris. 10-50-100f.

Solen ensis, Zin. B.-L, litt. Modiola marmorata, Forbes. B.-L,
strigillatus. L., litt.—10 f. litt.—40 f.

Saxicava arctica. Litt—160 f. Pecten tigrinus. B.-L., 10-100 f.
rugosa. Br. & L., 6-20 f. Sowerbyi.
fragilis. — pusio. Litt.-90f.

Syndosmya prismatica. B.-L.,3-100 f. | Anomia ephippium. B.-L.., litt.-160f.
Leda pygmza, Phil. EH. & W.B., L.,
25-50 f.

It is evident from the foregoing list that the. Edeghem fauna is
referable generally to a much deeper bed than the Scaldésien. This
consideration by itself shuts out such comparisons as have been
made; things so unlike as the assemblages of fossil shells from very
different ranges and conditions of sea-bed can only be compared for
the purpose of obtaining a knowledge of what those depths were.
Our acquaintance with the distribution of marine species over deep-
sea beds is as yet imperfect, but we know that it has its peculiar
facies ; and geologists have not sufficiently regarded this, hence much
erroneous generalization. It is well observed by Mr. J.G. Jeffreys*:
“It is obvious that negative evidence of the occurrence of any species
(and especially of those which inhabit deep water) in any given area
of sea is inadmissible; and naturalists do not differ from logicians
or lawyers in rejecting such evidence.” The peculiar forms of the
«‘ Crag Noir” could not possibly occur in Scaldésien beds, in respect
of their conditions of existence, though they should have been inha-
bitants of the same sea at the same time. The occupation of the
North Sea area by the true Crag fauna was not of lengthened duration,
nor does the fauna itself indicate that change in time which is so
clearly to be traced in the accumulations of long periods, whether
Paleozoic, Secondary, or Nummulitic. The Crag is not a formation,
but merely a single stage in the Kainozoic series.

3. Denudation.—The extent to which portions of the rock-forma-
tions have been removed, and the character of the surface denuda-
tions, are amongst the most interesting of the geological phenomena
of Belgium. Such is the denudation which occurred antecedently
to the Cretaceous series, and again before the Nummulitic. For the
present I would call attention to that which followed the completion
of the Crag-sea beds, because the evidence is very striking, and has
a bearing on some views recently put forward by English geo-
logists, to the effect that there is evidence of continuity and un-
broken marine conditions, from the Suffolk Crag upwards into the
Boulder-formation.

® Ann. and Mag. Nat. Hist. ser. 2. vol. xvii. p. 168.

246 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 24,

Abundant illustration might be derived from our own East Ang-
lian area to controvert this view, and prove that a great break and
a long interval of time intervened between the Crag beds and the
Boulder series, during which the North Sea was a terrestial area.
The Belgian evidence bears most on the length of the interval or
the lapse of time.

Over the whole of the broad area of the Scaldésien, Diestien, and
Boldérien systems of the map of Dumont the formations are seve-
rally at present represented only by isolated masses or patches:
away from Antwerp, and as the country rises southwards, these
occur. as the cappings of hills, or ridges. These sandy strata, which
perhaps may have admitted of easy denudation, must, from their
composition, have extended from place ta place; and what now re-
mains is not a thousandth part of what once was. In the case of
the valley of the Dyle, by Louvain, the denudation has extended down
to the Bruxellian beds of the Nummulitic series to a depth of 100
feet; and the completeness with which all the materials have been
removed is well seen in the slope of the hills, as also on the level,
along the railway cutting. The denudation about the Bolderberg is
of nearly like amount as at Louvain.

In these cases, as in that of Schelle, the loss and Campine sands
were spread out after the denudation of the Crag-sea beds; and as
these belong to the later portion of the glacial period, the denudation
of the country must be referred to some intermediate stage *.

4, Variation in Depth._—The movements of elevation and depres-
sion of the water-level which the North-Sea area experienced during
the Crag period, are very simple, and so far are in harmony with the
apparent short duration of that period.

The chalk flints, and the Septarian blocks derived from the sub-
jacent Rupellien beds, which also occur elsewhere at the base of the
Diestien system (Kdeghem) are the remains of shallower water con-
ditions than such as followed, or are proofs of depression.

Both on our own Suffolk area, as on that of Belgium, the change
indicated from the Red Crag to the Bryozoan, and from the Scaldé-
sien to the Diestien, was of diminished depth, or is evidence of
elevation. Its subsequent emergence was in the same direction.

The earliest condition of the Crag-sea area here indicated is sup-
ported by a study of the list of shells given by Mr. Nyst, as obtained
from the gravel bed at the base of the Diestien system at Edeghem *.

The Faluns of Touraine have experienced an amount of denudation
such as is presented by the Belgian Crag. M. d’Orbigny has made
this remark with respect to the first-named formation, that removal
to so great an extent should have happened to synchronous accumu-

* Considered with reference to a line of section from Fort 2. towards the
North citadel, the whole of the Crag series has been planed off from N.E. to
S.W., so that lower beds come to the surface; and this has happened twice :—
1. during the Crag period, when by diminution of depth the deeper sea-bed was
denuded, and covered up by the Scaldésien; 2. when its general surface was
eroded and removed.

t Bull. de Acad. Roy. de Sciences de Belg. sér. 2, vol. xiii. p. 29.

!

1866. | GODWIN-AUSTEN—BELGIAN TERTIARIES. 247

lations, though somewhat distant, is curious as a coincidence, but in
both cases it perhaps may be explained by the inconsiderable thick-
ness, as also the loose materials, of the two formations.

IV. Newer Karnozotrc.

1. Caillou Ardennais.—In the sections about Antwerp we seldom
failed to detect the thin line of quartz pebbles, to which the Belgian
geologists have called attention, as underlying the Campine sands.
They were here very small, few in number, but perfectly rounded ;
they have been derived from the quartz veins of Paleozoic rocks.
These are the Caillouw Ardennais of M. Omalius, and came originally
from that ridge or axis. As compared with other places to the
north and east they have evidently at Antwerp reached their ex-
treme limit of dispersion*.

In the section at Schelle the quartz pebbles serve to separate the
Campine sand from the older sandy accumulation ; but for these the
line might easily escape detection, so closely do the surface-sands
resemble the Crag sands beneath. At this place it is evident that
Campine sand has been spread over the country since the denudation
of the Crag, as at either end of the section it rests on the surface of
the Rupellien clay, and in this position the quartz pebbles are mixed
up with the chalk-flints which originally occurred at the base of the
Crag, and still remain en place.

About Hasselt the quartz pebbles occur in great abundance and of
large size; with them are chalk-flints, somewhat less water-worn.
Towards Maestricht the quartz gravel, as seen in the railway banks,
underlies a considerable thickness of argillaceous sand; the accu-
mulation increases in thickness as it approaches the line of the
valley of the Meuse, ending abruptly at a considerable elevation
above the present level of that river, which has deepened its course
out of these gravel beds.

From Hasselt towards the Bolderberg the plain presents a con-
tinuous spread of siliceous sands, overlying coarse quartz shingle
with flints. These sands and gravels end off at the base of the
Bolderberg ridge.

Quartz pebbles, beneath léss, occur in the high ground above Liege
on the north, as also north of Namur, both on the surface of the
Carboniferous limestone, beneath the léss, as also in the wide

fissures of those rocks. Wherever patches of Nummulitic sands

occur (Bruxelles beds), the quartz shingle separates the older sands
from the loss.

At Dinant, in the Condroz, the quartz shingle occurs everywhere
over the surface on the high ground; and lastly we met it in the
fissures which have been enlarged into the caves of Furfooz.

These caves occur in a mass of Carboniferous limestone overlook-
ing the river Lesse, a tributary of the Meuse, and taking its rise in
fie high ground of ne Ardennes, near St. Hubert.

* IT did not notice any quartz pebbles on the summit of the hill east of
Louvain.

248 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

In the first cave, which is established on a line of fracture of the
limestone, enlarged by the passage of water, the general order of the
accumulation which occupies the lower portion, is as follows (as
traced for me in my note-book by M. Dupont; a layer of “argile
smectique” of M. Dupont, next to the limestone rock, is merely the
product of the decomposition of the impure limestone) :—

‘a A thick accumulation of limestone talus, from the face of the
cliff.

2. Loamy sand.

3. Rounded quartz pebbles.

Beds 2 and 3 extend back into the cave, sloping upwards.

Fig. 3.—Section of the deposits at the entrance of the Furfooz Cave.

. Angular débris—Argile a blocs anguleux.
Stalagmite.

Sandy Clay. Bear and Reindeer.

. Shingle—Cailloux Ardennais.

Fluviatile sands. Beaver, &e.

sases

In the second cave, which is lower in the cliff, there is outside,
an accumulation of debris, beneath which, and passing into the
cave, are |

1. Sandy and marly beds, in which are a few angular blocks,
such as may have fallen from above whilst the bed was forming.
Lines of successive accumulation.

2. Bed of quartz pebbles, in layers, sloping outwards.

3. Sands, bedded, like river sand; remains of beaver.

The upper level of the pebbles in the second cave* is wholly below
that of the pebbles of the first cave; this cireumstance entirely dis-
connects the shingle from any alluvial action of the Lesse. Even
were the two accumulations at the same level, and had they been
lodged in these caverns by a river flowing down the valley at a very
high level, the arrangement of the pebbles would probably have been
the reverse of what it is.

The materials of beds 1 and 2 seem to have been introduced from
above ; and the only portion of the accumulation which has the cha-
racter of a fluviatile deposit is the sandy bed No. 3. Numerous
specimens of the shingle are scattered over the upper platform of the

* Ten metres above the level of the river.

.1866.] . GODWIN-AUSTEN—BELGIAN TERTIARIES: 249

limestone mass in which these caves occur, and show that the dis-
persion of the pebbles belongs to some broader agency than river-
action; whilst bed No. 3, with the remains of beaver, indicates that
antecedently to these conditions the valley of the Lesse was much
in the same state then as itis at present, or a line of river-drainage.

Bed No. 1 of the caves may be referred to the period of the loss,
and

Bed No. 2 to the Cadlloux Ardennais, which here consist of sisi
coarse shingle. »

There are no remains of any shingle banks at high levels along
the northern slopes of the Ardennes, which have been produced at
any Secondary, Nummulitic, or Tertiary period. Nor has the Paleo-
zoic series of Belgium been the source of any shingle met with in
the Nummulitic series of that country, the pebble beds in which
are wholly of chalk-flints. At low levels, as in the Tournay district,
there are great accumulations of quartz shingle at the base of the
Cretaceous series (Tourtia) ; but this is the direction in which the
Cailloux Ardennais are not met with. These Ardennais pebbles,
which have been distributed at a definite stage of the Glacial Period,
could not have been formed then, inasmuch as the region whence they
have been derived was not submerged, and the only other source
which suggests itself is that remarkable shingle bank which under-
lies the Devonian series of Belgium, in the Condroz, from Pepinster
to Nassogne and Couvin, along the Ardennes, namely, the “ Pou-
dingue de Burnot”’ of Dumont.

2. Glacial Drift—Detrital beds are in places interposed between
the Campine sands and the Crag-formation. We were conducted by
Captain Cocheteux to an interesting section exhibited in the outer
ditch of Fort No.4. The beds consisted of loose sands, loamy sand,
ending with somewhat coarse sands; at the base were pebbles of
white and black flint, and occasionally flint flakes (naturally formed) ;
there were also small white quartz pebbles; with these were bones of
Cetaceans, sharks’ teeth, Crag shells, and other spoil from older
Tertiary formations. All this material may be called local, such as
might have been derived from beds at no great distance; but there
were also many large ragged unworn chalk-flints ; these occurred
for the most part in the upper portion of the accumulation.

- The Scaldésien beds were much reduced in thickness at this spot,
so that the Campine sands and underlying detritus lay partly on
green Diestien’ beds; these last were also much eroded, and blocks
of the more tenacious portions had been cut out and caught up in
the detritus; the whole surface was scored out, in one case to a

considerable ‘depth.

_ This accumulation in all its circumstances was very like some of
the lower drift-beds of Suffolk; and enough was to be seen at this
place to warrant a reference to that stage of the East Anglian
marine drift-beds, which are represented by the sandy gravel- ‘beds
below or beyond the margin of the Boulder-clay.

Rocks of Scandinavian ¢ origin have not been met with beneath the:
Campine sands of this part, or indeed of any part of Belgium, nor:

VOL. XXII.—PARTIL ce

250 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 24,

did any occur tous. The transport of northern detritus southwards,
both over our own area and that of northern Europe, took place
during the:later Glacial period, and does not appear to have extended
to this part of Belgium.

3. Campine Sand.—Sables de la Campine.—In every section
which we saw about Antwerp, there was to be observed at the
surface a very uniform layer, which has been referred by the Bel-
gian geologists to that very remarkable sandy formation covering so
large a district on the confines of Belgium and Holland, the Campine,
or Kempenland, whence the “‘Sable Campinien ” of Dumont.

About the city of Antwerp this accumulation seems to be thickest
where the ground is highest, as outside the Malines Gate, in the
direction of the roads to Schelle and Boom by Fort No. 7. The
cuttings going on in this direction, beyond the “ Enceinte,” show
good sections, six feet and upwards in thickness, of fine sand; though
where the soil is moist, the beds have much the appearance, and
even character, of some of the buff-coloured Loss of Brabant.

It is noticed by Dejardin that the limited area on which the city
of Antwerp stands is bare of this formations “Cette ville a du
former une ile dans la mer Campinienne.”’

No fossil remains of any kind have ever been met with in this ac-
cumulation.

These sandy beds extend from Antwerp over the Campine, and
thence into North Holland; they form for the most part a barren
tract, which the Belgian Government has striven hard to bring into
cultivation, with only partial success, owing to the extreme lightness
of the sands, which are easily blown about, and are constantly
shifting. |

The superficial sands of Hasselt, towards the Bolderberg and
Beverloo, belong to the Campine formation.

The manner in which this covering of sand follows the rise of the
country from north southwards, overlapping all older formations, and
its inconsiderable thickness compared with its great superficial ex-
tent, forbid the supposition of accumulation by water, or of a ‘‘ Mer
Campinienne.” On the other hand, the aspect and uniform com-
position of these sands, the manner in which, when dry, they are
lifted about by the wind, suggest that they have originated as Dune-
sand, which has travelled inland from the coast-line of some former
condition of the North Sea.

The age of the “‘Campine Sands” has often been discussed. They
are now* very generally referred by Belgian geologists to the “ Sy-
steme Diluvien.”

Though the true Campine sand has never been found to contain
animal remains of any kind; it overlies a surface with Elephas pri-
magenius. Itis certainly older than the Polder-mud deposits, and

* M. Omalius, on the consideration that at Antwerp the Campine sands con-
form to the Crag, is disposed to refer them to that formation. The Antwerp
sections show very clearly that those sands have been spread out since the gene-
ral surface of the Crag sea-beds has been extensively denuded; occasional con-
formity is a mere accident.

1866.] GODWIN-AUSTEN—BELGIAN TERTIARIES. 251

their equivalents, the peat-growths. However, there may still be
a great range between these extreme periods.

In like manner the Loss overlees the gravel beds in which the frag-
mentary remains of the great Pachyderm fauna occur.

Both the Campine sands and the Loss are subsequent accumula-
_ tions to the Ardennes quartz pebbles; but the occurrence of these
pebbles at the base of both does not necessarily connect them with
either, but it suggests that these two accumulations must be nearly
of the same age; and such, it seems, was M. Dumont’s latest view.

The presence of quartz pebbles in the detrital beds at Fort 4 sup-
plies another link to the chronology.

To what extent the surface of Belgium was submerged during the
Glacial Period cannot easily be determined, owing to the thick
coverings of subsequent date. Antwerp probably marks very nearly
its marginal line; and this agrees very well with the range of the
true “Boulder Formation” with northern rocks extending from
Arnheim to Groningen and into Hanover. If the fine sands (Zand
diluvium) which in North Holland form the overlying portions of the
Boulder-formation, be connected with the Campine sands of South
Holland and Belgium, they present a line parallel with that of the
Boulder-coast ; and then, as all their characters would indicate, they
might be the blown sands from the marginal beds of that period,
and of that stage of it when the Northern Hemisphere began to re-
emerge—a process which took place from south to north.

4. Loss.—During our visit we came upon good illustrations of the
superficial layer known in Belgium as the “ Limon de Hisbaye.”

It occurs at considerable elevations to the north of the Sambre
and Meuse, along the line from Liege to Namur and north of
Charleroi; but it does not rise to corresponding elevations on the
south of those rivers, on which side, though of great thickness, it is
at low levels. During the excursion of 1852 we saw a thick ac-
cumulation, with Succinea oblonga and Pupe, at Audregnies ; and
this year I saw good sections of it, both above Namur and about
Gembloux. From Liege westwards the Loss may generally be sepa-
rated from any beds it may overlie by the presence of a seam of
quartz pebbles. .

The land-shells cited above are not commonly met with, but they
- Increase in frequency towards the line of the Ardennes. The Léss in
its arrangement, when in great masses, shows that it has been de-
posited by water. The‘Sable de Campine” and the “ Limon de
Hisbaye” form, as was long since said by M. Omalius, the “ man-
teau de la Belgique.” The two accumulations have never been
noticed to overlap, they rather pass into one another, along a line
from west to east, the sands being to the north and the fresh-water
Loss to the south. The opinion of M. Dumont, that they were
somewhat synchronous, has been alluded to. -

5. Polder Mud.—The Polders, or brackish-water mud-flats of
the low coast of Belgium and Holland reach up on either side of the
Scheldt as far as Antwerp. This is the most recent sedimentary
formation we saw, consisting of blue mud, as may be seen in the

T2

252 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 24,

banks of the Scheldt and on the slopes of the broad ditch of the north
citadel, where it is full of small shells of the common Cardium and
Scrobicularia ; land and fresh-water shells also occur. The whole
district of Zeeland, as the name implies, is of this sea mud. The
‘“‘argile d’Ostende” is of the same age, with the same shells. Along
the whole of this coast the Polder-mud passes below the present sea-
level, as may be seen occasionally off the Ostend coast at low water,
where the compact mud resists the action of the sea. The composi-
tion of the Ostend Polders differs a little from that of those to the
north, in the large proportion of calcareous matter, which has pro- —
bably been derived from the waste of the chalk. The Zeeklei of
the North Holland coast is also Polder.

The Polder formation indicates a change of level, or of releamiee
elevation of the land, of small amount, but of remarkable unifor-
mity, from Ostend to whe coast of Heecer it also corresponds with
alluvial accumulations and mud flats to be met with in suitable
situations about our own coasts, whether of the English, Irish, or
German Seas.

The Dunes, or great sand hills, along the coast south-west of
Ostende, as well as those of North ‘Holland, have all been accumu-
lated on the Polder mud, and since the charise of level.

The Polder mud differs from the accumulations of the paces
coast-line of Belgium and Holland, which consist of fine siliceous
sands, and must have been deposited in brackish water lagoons,
into which the rivers discharged, and which were separated from
the open sea by sand-banks.

6. Terrestrial Surface.—From specimens in the Antwerp Misenta
it would appear that when a breach is made in the Polder mud, a
terrestrial surface with large trees is exposed. The like was met
with in the excavations for the new docks, consisting of rich peat.
This old land-surface is to be seen at low water, beneath the Polder
mud. In like manner it underlies the Zeeklei of Holland; and
much, probably, of the surface of peat or old fen of Belgium and
Holland (Hooge Veenen), above the level of the Polders, is merely an
upward and inland extension of the same surface of plant-growth.

In the Antwerp collection are some Mammalian remains, which
were obtained at West Capellen, the extreme seaward point of the
Island of Walcheren, when the sea had made a breach there. Mr.
Busk recognized the perfect lower jaw, tibia, and other bones of a
young Elephas primigenius, also two teeth of Rhinoceros tichorhinus.

Belgium for the most part belonged to that particular zone which
was a limit to the area of the last great north cireumpolar depres-
sion ; and its superficial geological phenomena belong to the subaerial
agencies of the glacial period; such are the “ Cailloux Ardennais”
and the Loss, as well as the Sables de Campine. /

At some time antecedently to that of greatest submersion, the
line of Artois, and of the Ardennes (like our own Wealden), had been
placed at a much greater elevation than at present, with respect to
Brabant and the Hesbaye ; the position of the Liss shows this. The
surface. may have been brought to its present levels partly by de-

1866.] -GODWIN-AUSTEN——BELGIAN TERTIARIES. 253

pression of the line of the axis of the country, partly by the eleva-
tion of the district north of it (Brabant and Hesbaye); but had the:
valley of the Meuse existed as it is now, at the time of the dispersion
of the Ardennes pebbles, or of the accumulation of the Léss, it:must
necessarily have been choked by them; but the very reverse is the
case, and that valley (which is a line of fracture) may be safely
pointed out as the line of one of the changes of relative level which
have happened since the later Glacial Period.

- Should the supposition be correct as to the source of the Arden-
wile pebbles, the disintegration of the surface by which the pebbles
of the “‘ Poudingue de Burnot”’ were set free along the slopes of the
Ardennes, must be referred to the period of greatest elevation, of
cold, and great river-courses; the larger and coarser accumulations
connected with the line of the Meuse from Liege having been brought
- down by the Ourte and the Ambléeve. The quartz pebbles of the

line of the Meuse having come from the upper sources of the Lesse,
are of less size, ee as the streams are smaller. :

In like manner the Loss was the deposit of the turbid waters which,
at the break up of every winter, periodically accumulated over the
low area (now part of Brabant and the Hesbaye) between the slopes
of the Condroz and the Dune sands from the coast.

Viewed in this light, the Belgian area seems to offer some very
interesting illustrations of the varying conditions of the last great
Glacial Period.

7. Sangatte Beach. BRehane leaving the geological phenomena be-
longing to this period, I would briefly call attention to a few points
connected with the section of the coast from Sangatte,—a section of
very great interest, relative to which Mr. Prestwich has recently
given a second paper, and which we visited together.

At the base of a vertical cliff of chalk there is a coarse shingle
beach, and a little in advance of it are horizontal sands, with a few
flint pebbles ; ; these are of marine origin, and the section corre-
sponds with that at the base of the subaerial beds at Rottingdean
and Brighton.

Above the marine sand and shingle is a black band, occasionally
very strongly marked, the evidence of an old terrestrial surface,
The level of the old coast-line was very little above the present, but
subsequently there must have been a rise, to what extent cannot
here be determined; but the subsequent accumulations all indicate
subaerial conditions.

Above all are blown sands; next below these, near Sangatte, is
an angular débris of flints, with blocks of ferruginous sandstone, fol-
lowing the coast-line ; layers of Loss succeed, with occasional flints,
also land shells. The thickness of the beds of sandy Loss and of
loam (as of the angular materials) increases in the direction of the
chalk hills, and at last the mass passes by alternations from earthy
Loss to chalky marl, and seams of chalk nodules; these become a’
chalk rubble; and angular blocks of chalk of considerable size,
have been accumulated against and at the foot of the old cliff, and:

above the marine beds.

254 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

All these materials have been swept off the northern slopes of the
chalk hills. The thickness of the accumulation is remarkable, as
also is the distance to which the materials have been carried for-
ward; and may serve as a measure doth of the duration and in-
tensity of the Glacial Period.

The great plain of flint shingle which may be observed about
Calais, and extending inland, belongs to the same level as that at
the base of the old cliff, and is probably of the same age. The beds
of chalk-marl which underlie the peat in the direction of St. Omer
are also of the age of the Loss of the Sangatte section; and the
details of that section may be assumed with respect to the base of
the chalk range on the north, so far at least as the shingle extends.

The character of the subaerial glaciation of the south ‘slopes of the
Ardennes and axis of Artois is the same throughout; and if the
phenomena are on a broader scale when they are in connexion with
the higher parts of the range, the history of the period is perhaps
more completely indicated in the Sangatte section.

February 7, 1866.

Thomas Belt, Esq., Prince of Wales Mine, Dolgelly; Thomas
John Bewick, Esq., Haydon Bridge; Thomas Forster Brown, Esq., |
H.M. Deputy Gaveller of the Forest of Dean, Coleford; J ohn F.,
Campbell, Esq., of Islay, Neddry Lodge, Kensington ; William Cory,
Esq., 4 Gordon Place, W.; Anastasius Gowdas, M.D., Athens;
William Frederick Cowell Stepney, Ksq., 9 Bolton Street, Piccadilly,
W.; and John Young, M.D., Geological Survey of Great Britain,
Jermyn-street, 8.W., were elected Fellows.

The following communications were read :—

1. On the Formation of Laxr-Bastns in NEw ZEALAND.
By W. T. Locxz-Travers, Esq.

[In a letter to Sir Charles Lyell, Bart., F.R.S., F.G.S.]

In consequence of reading a notice in the 6th volume of the ‘ Intel-
lectual Observer,’ p. 461, of what I presume to have been a com-
munication from Dr. Haast to the Geological Society, in reference to
the formation of lake-basins in this country, and of my inability to
subscribe to the views of Dr. Haast, I venture to submit my reasons
for dissenting from them.

My observations have been chiefly directed to the great mountain-
system named by me the “Spencer Mountains,” which occupies the
centre of the block of country constituting the Provinces of Nelson
and Marlborough, in the Middle Island. The highest point of the
range is Mount Franklin, estimated at 10,000 feet, whilst around it
are several lower peaks, averaging from 7000 to 8000 feet.

A number of the largest rivers in the northern part of the island

1866. | _- LOCKE-TRAVERS—LAKE-BASINS. 255

Sketch Map of parts of the Provinces of Nelson and Marlborough, in
the neighbourhood of the Spencer Mountains.

oy
oe

j BLIND BAY ye ?
: ee

BR. MOTUEKA Leoypp ¥ 4
ens dp
erty

Me

- 256 PROCEEDINGS OF THH GEOLOGICAL SOCIETY. [Feb. 7,

have their sources in these mountains, flowing from them to the
north, south, east, and west. Amongst the rivers on the northern
side of the range is the Buller or Rotoiti flowing out of Lake Arthur,
and the Roturoa flowing out of Lake Howick. On the south side of -
Mount Franklin is the River Waiaw‘or Dillon, and the Clarence, which
flows out of Lake Tennyson. It is chiefly to the above-named lakes
and the valleys of the rivers that I shall refer.

A line of: road leads from the town of Nelson, in Blind Bay, to a
place called the “Old Pass,” nearly due south of Ben Nevis, and
continues thence past Lake Arthur and along the course of the
Rotoiti and Buller rivers to the junction of the Roturoa with the
latter. .If from this point a line be drawn to the source of the
Todmor river (a feeder of the Motueka) and continued down the
eastern bank of the latter, it will again reach the sea.

Stretching along the northern bank of the Rotoiti river, and com-
mencing nearly due north of Lake Arthur, is a range of hills marked
as being 2324 feet in height. Now this range of hills, and all the
spurs running north from it within the space above described, are
composed of post-Pliocene boulder-beds, gravels, and sands, mm ne
degree cemented, very little inclined in stratification, and im many
places exhibiting perpendicular sections several hundred feet high,
particularly wherever the foot of the hills has been washed by rivers.
The materials are all water-worn, and exhibit the common appear-
ance of river or beach shingle; they overlie older Tertiary rocks,
to which Dr. Haast assigned a Miocene age; but I am inclined to
think he is in error in this respect, looking to the great similarity
between most of the embedded fossil shells, and the shells now living
in the adjacent seas.

These post-Pliocene beds extend northward as far as “ Wakefield,”
terminating abruptly in cliffs, the bases of which have evidien iy been
formerly washed by the Wairoa river.

A little to the westward of the north-western corner of Lake
Arthur is a small stream flowing into the outlet, and some miles
further south a river called the Howard flows through a valley*
bounded on both sides by hills composed of extremely loose material.

Now the whole valley, nearly a mile and a half wide, between the
the margin of Lake Arthur and the above-mentioned range of hills
in front of it,is occupied by a huge moraine, the extremity of which
rests upon the flanks of these hills, stretching right and left along
their line in the direction, on the one side, of the Old Pass, and on
the other, of the course of the Rotoiti. Many of the blocks of rock
composing this moraine measure from 15 to 20 feet square, and all
are composed of débris from the ranges on each side of the lake,
affording sufficient proof that they were deposited by a huge glacier
which formerly occupied its site.

In the direction of the Old Pass the moraine does not stretch fur-

* The hills lying between this small stream and the Howard are also com-
posed of the same Post-pliocene boulders, gravels, and sands as those above
mentioned, In effect the River Rotoiti runs, as far as its confluence, with the
Howard.

1866. ] LOCKE- TRAVERS—LAKE-BASINS, 257

ther than the watershed beyond the Rotoiti and the Wairau, whilst,
on the course of the Rotoiti river, it stretches for several miles down
the valley, and we find erratics on the flanks of the hills on both
sides nearly as far the Howard. At this point the Rotoiti enters
the granitic zone of Mount Murchison, isolated peaks of this granite
appearing on the north side of the river “ rising” (in the words of
Dr. Haast, in his ‘ Report on the Geology of the Province of Nelson ’)
<< through the alluvium ;”’ but the great mass of the hills stretching
along the north bank of the river as far as the junction of the
Roturoa is still composed of the before-mentioned Post-pliocene
formation. |

Lake Arthur lies between a great spur of Mount Robert on the one
side, and the foot of the St. Arnaud Range on the other ; its principal
feeder rising in Mount Travers. Now, this lake is several hundred
feet deep, the depth gradually increasing from its upper end until
you approach its broadest part, when it again begins to shoal. In
front of it lies the great moraine before referred to, rising about 100
or 150 feet above the level of the water, the outlet having made its
way through this at the north-west corner of the lake, exhibiting a
section of from 100 to 120 feet in height.

Passing on now to Lake Howick, I may mention that on tho
flank of the granite range between the Howard and this lake, I
found Tertiary strata containing thin bands of lignite. These beds
were brought to light by a large side cutting, made during the con-
struction of a road, long after Dr. Haast had visited the district, and
were very likely then to have escaped his observation, as the whole
district is densely wooded, and the surface so encumbered with dead
and living vegetable matter, as entirely to conceal the soil, except
where actually cut into. Dr. Haast, in the report before alluded to,
refers to the existence of seams of lignite in this neighbourhood,
stating, however, that “he had not seen them in situ, but had found
large pieces lying upon the shingly banks of the Howard.”

On descending into the valley of the Roturoa (which is densely
wooded throughout) I found it was filled, in front of the lake, with
moraine matter derived from the mountains on each side. I did not
travel down the valley to the junction of the outlet with the Buller,
but I was informed by the solitary ferryman at the lake that it was
“very rough,” and full of “ big stones,” from which I conjectured
that it was probably filled throughout with ice-borne matter. The
~D’Urville and Sabine rivers, the principal feeders of the lake, flow
through frightfully rugged valleys. I ascended the range between
them to the height of nearly 8000 feet, but being alone I did not
care to attempt Mount Franklin. I saw enough, however, to satisfy
me, that enormous glaciers formerly descended the valleys of the
Sabine and D’Urville, and after uniting at the extremity of the
dividing spur, filled the site of the lake. I had no opportunity of
examining the range of hills on the north bank of the Buller, oppo-
site the mouth of the Roturoa, so that I am unable to say whether
moraine matter occurs on.their flank, in the same manner as on the
flanks of the hills in front of Lake Arthur. -I think it extremely

258 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

probable, however, looking to the course and general appearance of
the valley of the Roturoa, that the glacier stretched as far as the
Buller, filling the present valley with moraine matter as it receded,
becoming stationary for some time near the present margin of the
lake where the moraine attains its greatest height.

Lake Howick, in its deepest part (rather less than halfway up),
is upwards of 1000 feet deep, and again shallows as you approach
the moraine. The outlet has made its way through the moraine,
exhibiting a section about 30 feet in height.

Of course it 1s impossible to say to what depth the moraine matter
in front of these two lakes extends ; but I cannot help thinking that,
if it could be traced downwards, we should find it lying on the same
foundations as the post-Pliocene beds above referred to,—from which
we might conclude that, enormous as the period must have been, the
sites of these lakes were occupied by ice when the period of depres-
sion commenced during which those beds were deposited, and so
continued for some time after the reelevation of the land above the
level of the sea. At all events it appears to me, in view of the facts
above mentioned, impossible to admit that these basins owe their
existence to the scooping power of ice. I should gladly have de-
voted a longer time than I was able to give to the examination of
this district at the period of my visit to it, but the fact was, that my
son and one of my men had several of their toe nails washed off, and
our hands and bodies were so stained that it took nearly three weeks
to get them clean again. The utmost devotion to science was scarcely
proof against such weather.

I will now mention the facts observed by me in the valleys of the
Dillon and Clarence, as these valleys present features of exceeding
interest in.connexion with former glacial action. As a general rule
in this country, in valleys which have never been occupied by glaciers,
the spurs of the ranges on each side interlock ; whilst in those which
have been occupied by glaciers we constantly find the points of the
spurs on one side or other of the valley cut off, the faces of the spurs
then being A-shaped, and rising at a very steep angle. I have ob-
served the latter feature to obtain in all the valleys in which I have
found old moraines, and I think it may be a good guide in deter-
mining the longitudinal extent of former glacier action.

The upper part of the river Dillon flows through a valley now
occupied by me as a cattle-station. Now, stretching across the
valley, from the mouth of the “‘ Henry” to the range on the eastern
side of the river, is a huge moraine, filling the valley for nearly
three miles of its length. This moraine rises about 100 feet above ©
the level of the valley on its upper side. After the retreat of the
glacier, and until the river, aided by the waters of the Henry, had
' worn a channel through this moraine, the upper valley was filled
with water, and the margin of the lake so formed, as seen on the
moraine, about 30 feet above the level of the valley, is as fresh as if
it had only been emptied a week ago. About 14 miles up the valley
is another and much smaller moraine, showing where the glacier had
rested during its retreat.

1866. | " LOCKE-TRAVERS—LAKE-BASINS. 259

The glacier which deposited the lower moraine must have been a
stupendous one, for there are erratics and “ roches moutonnées” on
the sides of the mountains, to the height of 1000 feet and upwards.
The valley is about a mile wide at the moraine, increasing in breadth
opposite the “‘ Ada” and ‘ Christopher ” rivers, the valleys of which
were evidently occupied by branches of the great glacier. The length
of the main glacier was about 23 to 24 miles, that of the Ada branch
about 8, and that of the Christopher branch 5 or 6. The mountains
on each side of these valleys are extremely steep, and the main valley
now rises about 35 feet to the mile.

Looking to the appearance of the valley below the moraine, there
is no doubt that the glacier formerly extended as far as the junction
of the Dillon and Hope, but I did not see in the upper part of the
latter river, or in the Dillon below the junction, any traces of glacial
action. About ten miles below the junction the waters of the united
rivers debouch upon the Hanmer Plains, and thence find their
way through a rocky gorge into the Hurunui Plains. On the sides
of the mountains bounding the Hanmer Plains, south of the river,
we find a succession of old terraces, the uppermost of which is fully
700 feet above the general level of the plains. The lowest terrace
rests upon the rock through which the river now flows, upon which
it forms a capping of considerable thickness. I conceive that the
material of these terraces was deposited during the same period of de-
pression which gave rise to the Post-pliocene boulder beds and gravels
on the north side of the range, and that the now rocky channel of
the river has been excavated since the reelevation of the land.

Reverting to the great moraine above referred to, [ found that
the main river, aided by the Henry, had cut a way through the
moraine matter, exhibiting sections from 80 to 100 feet in height.

In its course through the gorge below the Hanmer Plain, the
river has cut a channel through solid rock 120 feet deep below the
level of the lowest shingle terrace, showing the enormous wearing
power of water charged with sediment, even though flowing on so
apparently slight a fall as 35 feet to the mile.

There is, I conceive, every probablity that the valleys of the
Dillon and Clarence were filled with ice at the same time as the
present sites of lakes Arthur and Howick, although the bed of the lake
formerly existing behind the moraine dam of the Dillon has since been
filled up, the river-borne matter being banked up against the sloping
face of the moraine. What the original depth of that lake may
have been it is impossible to say ; but there is no reason to suppose
that it may not have rivalled those on the north side of the chain.
I attribute the rapid filling up of this lake-bed to the facts, that the
mountains bounding the valley of the Dillon are exceedingly steep,
are composed of easily disintegrated sandstone, are very bare of ve-
getation, and present in many places for thousands of feet in height
and for miles in length, little else than avalanches of broken stone ;
whilst those which bound the Lakes Arthur and Howick are densely
wooded, are very much less steep, and are composed of granite and
other hard crystalline rocks.

260 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Rebo7z,.

Passing from the valley of the Dillon into that of the Clarence,
distant about six miles in a direct line, and running parallel to it
for some thirty miles, but fully 1000 feet higher in point of level,
we find Lake Tennyson, dammed in by a moraine which rises about
fourteen or fifteen feet above the level of the water. This moraine
stretches about a mile and a half down the valley, sloping very
rapidly. Ihad no means of ascertaining the depth of the lake ; but
I do not believe it exceeds 400 to 500 feet: at all events, there is
nothing to lead to the supposition that its bed is lower than the
foundations of the moraine by which it is dammed in.

In the case of these inland glaciers we have to assume that a
considerable body of the ice of which they were formed lay below the’
upper level of the terminal moraine; but this would not prevent the
water arising from the melting of the ice from escaping in the
same manner as that which flows from a retreating glacier.

' My knowledge of geology is not sufficiently great to enable me to
see any difficulty in supposing that ice may have existed in the
localities referred to during the enormous period required for the
‘deposition and reelevation of the above-mentioned Post-pliocene beds,
and this, therefore, I must leave to more competent judges ; but I
really cannot see anything to justify the opinion, that the lake-basins
owe their existence to the “scooping power of ice.”

I have confined my remarks to the lake-basins found among the
spurs of the Spencer Mountains, which, however, afford a fair ex-
ample of all the lake-basins north of the river Waitki. In fact, I
firmly believe that all the lakes which lie in the valleys of rivers
debouching on the Canterbury Plains owe their existence to moraine
dams, which have the same foundations as the Post-pliocene shingle
of which the plains themselves are formed, and that, therefore, the
sites of those lakes were occupied by ice at the commencement of the
period of depression, and so continued for some time after the re-
emergence of the upper part of the plains above the level of the sea.

2. On the OccuRRENCE of DEAD Lirrorat SHEris wm the BED of the
German Ocuan, forty miles from the coast of ABERDEEN. By
Rozsert Dawson, Esq.

[Communicated by T. F. Jamieson, Esq., F.G.S.]
(Abridged. )

Tur bank called the “Long Forties,” from 35 to 40 miles from
land, extends from opposite Kinnaird’s Head in a direction nearly
parallel to the shore. Inside of this bank the depth varies from 90
fathoms at the northern end to about 50 fathoms opposite Aberdeen.
Being becalmed we dredged on this bank for a considerable time in
36 fathoms, 40 fathoms, and 42 fathoms, on a bottom of broken shells
and shingle. I remarked at the time that these dredgings contained
none of the Arctic fossils found so plentifully in every haul when:

1866.]. : ' JAMIESON—CAITHNESS. 261

dredging nearer the shore, and from this I inferred that the fossili-
ferous bed, which seems to stretch along the coast at a distance of
from six to fifteen miles, does not extend beyond this deep water to
the «‘ Long Forties.”” On examination of the materials brought up by
the dredge from the top of the bank, there were found shells of the
following species in a worn and semi-fossil condition, namely :—

Purpura lapillus, one specimen.

Titorina rudis, one specimen.

Solen siliqua, two specimens.

Mytilus edulis, one large broken valve and several fragments of
smaller specimens.

Before it occurred to me that these fragmentary fossils might be
interesting in a geological point of view, the greater part of the
dredgings had been examined. It is quite possible, therefore, that
_ other specimens may have escaped notice.

Now as Litorina rudis is generally found on rocks above high-water
mark, and never beyond low-water, and as all the other species are
highly characteristic of the shore, or very shallow water, it seems a
fair conclusion that at the period when these were living, the relative
levels of land and sea were very different from what they now are,
and that the bank had then formed the shore of the German Ocean.
If only one specimen had been found it might have been accounted
for by some of the many accidents which occasionally bring even a
foreign shell into the dredger’s bag; but four species having been
found in the course of one day’s dredging, it appears very probable
that they lived and died where they were found.

3. On the GLACIAL PHENOMENA of CAITHNESS.
By T. F. Jamizson, F.G.S.

ConTENTS.
1. Introduction. 7. Relation of the Caithness Drift to
2. General distribution of the Drift, that of the rest of Scotland.
its colour, texture, and contents. 8. Its place in the history of the
3. Character of the Stones imbedded - Glacial period; reference to
in the Drift. sections at Invernettie, King-
4. State of the Shells. Edward, and Arran.
5. The Glaciation of the Rocks and 9. The Post-glacial period in Caith-.
Boulders. ness.
6. Absence of Moraines and Gravel- 10. Appendix, with two tables con-
hillocks. taining lists of shells, &e.

1. Introduction.—In August 1865 I paid a visit to Caithness, in
order to study the last geological changes in that north-eastern
corner of Scotland. Mr. Peach has lately given us an excellent
account of the fossil-contents of its glacial beds, from which he
enumerates seventy-five species of Mollusca, besides various other
forms of Invertebrata. The object, however, of my visit was not so
much to look after the fossils as to satisfy myself about the conditions

262 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 7,

under which the beds containing them had been accumulated, and
to compare them with those of other districts with which I was
already acquainted.

In the neighbourhood of Glasgow, and along the east coast from
Aberdeen to Edinburgh, we find the beds containing Arctic shells
lying on the top of a rough boulder-clay destitute of such fossils;
and these marine fossiliferous beds are often of great depth and
finely laminated, presenting all the features of tranquil and regular
deposition. The remains of mollusca and starfishes in them are, in
many instances, quite entire and uninjured, as if they had been gra-
dually enveloped in the fine mud in which the animals lived and
died, while the crust of large barnacles on some of the stones points
to a like stillness of the sea-bottom. In Caithness nothing of this
sort has been observed; no distinction has been made of a rough
boulder-clay destitute of fossils and an overlying marine fossiliferous
bed; the shells, according to all observers—Dick, Cleghorn, Hugh
Miller, Peach, and others—are described as being scattered in a
broken state all through a mass of rough boulder-clay, and no such
thing as a bed of tranquilly deposited marine sediment containing
entire shells has been reported. This seemed to me to indicate
that the conditions under which the glacial beds of Caithness were
accumulated must have differed in some way from those that pre-
vailed in the other districts, and I was therefore desirous of studying
the locality in order to make out, if I could, the cause of the
difference.

2. General distribution of the Drift,rts colour, texture, and contents.—
Viewed from a distance, Caithness has the appearance of a bare
undulating plain, sloping very gently to the north and north-east,
and terminating in lines of rocky cliff which are battered by a rest-
less and stormy sea. Along the southern border of this plain there
is a fine group of hills, of which Morven (2331 feet), the Scarabins
(2048 feet), and the Pap of Caithness (1229 feet) are the most con-
spicuous; there are, also, some straggling heights of lesser impor-
tance along the western side of the county. These hills form a sort
of separation or boundary between the low district of Caithness and
the more mountainous region of Sutherlandshire. Geologically it is
a country of Old Red Sandstone. The hills just mentioned consist
of quartzose mica-schist and granite, on the flanks of which repose
thick masses of conglomerate and grit forming the base of the Old |
Red in this region. These beds of conglomerate and grit pass up
into a great series of thin-bedded shales, flags, and sandstones, gene-
rally of a dark-grey colour, which stretch away in billowy undulations
over the surface of the country to its north-eastern corner, as has
been well shown by Sir Roderick Murchison.

It is in the low troughs and winding hollows which form the
beds of the various streams that we find any quantity of glacial
débris; on the higher ground the rocks are either bare and devoid
of earthy cover, or hidden by a growth of peat and heather. Some
of these low tracts run across the country from side to side, as, for
example, from Wick to Thurso by way of Loch Watten, and between

1866.] JAMIESON——CAITHNESS. 263.
Fig. 1.—Sketch Map of Caithness, showing the boundary of the dark-
grey drift, and the direction of the glacial markings.

SCRABSTER

OUNNET Ho B

DUNCANSRY no

KEISS
SINCLAIR BAY

NN WICK

LYBSTER
2,8

SCARABINS DUNBEATH

=

= -

/ <= "=m acemensnee =”
seas

<y BERRIEDALE
ORD OF CAITHNESS

5 .10

os |

Scale of English miles.

-— Direction of glacial markings.
--.- Boundary of dark-grey drift.

264 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

Dunnet Bay and Sinclair Bay. Another low tract passes up the bed
of the Thurso water and along to the east coast by way of Dunbeath.
The drift is spread in sheets fillmg up these troughs and levelling
the irregularities of the rocky strata so as to impart a smoother and

softer outline to the surface. So far as I saw, it does not form irre- .

gular mounds and hillocks, neither is it very rough on the surface
with erratic blocks; it seems confined in a great measure to the
lower levels, thinning out at altitudes of 100 or 150 feet. The
thickness, therefore, varies much, being greatest in those depressions
which descend nearly to the sea-level. Thus at Scrabster harbour,
in Thurso bay, there are banks of it more than 100 feet high, and
in some of the troughs of the south branch of the Dunbeath water
it is nearly as thick. Deep masses occupy the hollow from Watten
to the Bay of Wick, and also stretch along the Thurso river into the
very centre of the county. There is also a good deal of it in the
bed of the Forss and at Lybster, but at the Freswick Burn it is com-
paratively thin. -In all these places it is of very much the same hue,
being of a deep leaden-grey or slate-colour, very dark when moist,
and considerably paler when dry, similar, in fact, to the colour of the
Caithness flags on which it rests. Occasionally the upper portion is
of a browner, more ferruginous tint, which may be owing to the
influence of the atmosphere, the percolation of surface-water, or to
some other cause.

Fig. 2.—Scrabster Harbour.

1. Unstratified pebbly clay with very few broken shells.
2. Old Red Sandstone.

The texture, however, varies a good deal in different places. At
Scrabster harbour, where it reaches a thickness of more than 100
feet, no difference can be perceived from top to: bottom ; it is just
the same at the base, where it is in contact with the ice-worn sur-
face of the subjacent rock, as it is 100 or 150 feet higher up. It
shows no stratification nor traces of gradual deposition. Itis a coarse
gritty mud, exceedingly firm and difficult to pierce, and thickly
charged with small stones, which are dispersed very uniformly
throughout all parts of the deposit. Pebbles of all sizes below that
of a man’s fist or foot are the prevailing dimensions, but stones of
from two to three feet in length also occur; I saw no great erratic
blocks. The stones are more or less worn and rubbed, and many of
them show the glacial scratches. A few small fragments of shells
are dispersed through all parts of the bank, from the bottom to
within at least 15 feet of the top, but are by no means common.
Such is the character of the section at Scrabster, and it is very much
the same along the banks of the Thurso water for several miles up

————

1866. ] JAMIESON—CAITHNESS, 265

its course; but fora mile or two above Halkirk pieces of shells are
more common, and occasionally an entire valve may be met with.
So thickly packed is this drift with small stony rubbish that in many
places almost every handful of mud contains several fragments.

Along the banks of the Haster Burn, near Wick, large stones are
more common in the drift, and there are even some considerable
boulders ; but notwithstanding the coarse stony nature of the deposit,
this is one of the best localities for fossils, fragments of shells being of
frequent occurrence dispersed in the unstratified rough stony mud;
and in the course of a single visit to this stream, in company with
Mr. Joseph Anderson of Wick, I got an entire valve of Astarte borealis,
and one or two specimens of Turritella and Natica nearly perfect.

At the south branch of the Dunbeath stream, the sections are
similar to those on the Thurso river, and pieces of shells about equally
common. In the bed of the Forss the drift 1s very full of stones, and
shells are exceedingly rare ; otherwise it resembles that of the loca-
lities just mentioned.

Fig. 3.—Section at Wick Bay.

(EEDA

A

cS ———

1. Reddish-brown clay with boulders.

2. Dark pebbly silt with broken shells.
3. Old Red Sandstone.

At Wick, however, it is somewhat different ; in the banks beside
the harbour (at Pulteney town) the drift is 50 or 60 feet deep.
The lowermost two-thirds of it are a sandy mud, or silt, of a very
dark grey colour, solid and firm as if much compressed ; and although
there are a good many small pebbles dispersed through it, yet they
do not form a large proportion of the mass, and there is an absence
of big stones. Fragments of shells are in many places not uncom-
mon, and are scattered through it in an irregular manner, not
occurring in horizontal lines or seams. There is, in short, no dis-
tinct stratification, although in some places there is an approach to
it, owing to patches of a more sandy nature occurring; it is an
unstratified pebbly silt, the greater part of the mass consisting of
fine sand. The upper part of the bank, on the other hand, is of a
browner, more ferruginous colour, much coarser in quality, with
more muddy sediment and few or no shells ; it is also full of stones
and large ice-worn boulders of sandstone, quartzose, mica-schist,
and granite, on which the glacial scoring is well marked. One of
these granite blocks is 12 feet in length. I cannot say . that
there is any clear sharp line of separation between this coarse upper
stuff and the dark siltier matter beneath ; for although in some places
the distinction is pretty well marked, in others they seem to gra-
duate into each ether. Where the rock rises in the cliff, the dark
silty portion thins out, and the coarse brown mud full of boulders
rests immediately upon the ice-worn surface of the Caithness flags.

VOL. XXII.—PART If, U

266 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

Fig. 4.—Section at Keiss Harbour.

E,

1. Reddish-brown stony clay.
2. Dark-grey pebbly silt with broken shells.
3. Sandstone, iceworn.

At Keiss harbour, which lies seven or eight milesfurther tothe north,
the character of the section is very much the same as at Wick.
The total thickness of the drift near the harbour is about 40 feet.
The lowermost 23 feet consist of an unstratified mass of dark sandy
mud, with a few broken shells and some stones dispersed through
it, which reposes directly upon the ice-worn surface of a red sand-
stone rock, without the intervention of any other deposit. The
scratches and grooves point N. 35° to 40° W., and some of the
imbedded stones are likewise scratched. The upper 17 feet of the
bank consists of a browner coarse mud with more stones, and, so far
as I observed, no shells. Although the lowermost sandy portion of
the drift at Keiss and Wick has no distinct stratification, it is never-
theless more like an ordinary marine deposit than what I saw in the
other sections throughout Caithness.

3. Character of the Stones imbedded in the Drift——The stones
imbedded in the Caithness Drift consist for the most part of the débris
of the Caithness flags—those beds which Murchison terms the middle
division of the Old Red Sandstone of this part of Scotland—and
accordingly the general hue of the drift closely resembles the pre-
vailing dark bluish-grey tint of these strata. There is, however,
always a mixture of other sorts ; fragments of quartzose mica-schist,
and granite occur, so far as I observed, very frequently in the drift
of all parts of Caithness. I noticed them at the Burn of Freswick,
which is only a few miles from Duncansby Head, also at Keiss, and
all about the neighbourhood of Wick, and along the whole of the
Thurso water. There are likewise generally some fragments of
sandstone and conglomerate, and occasionally one of hornblende-
schist; this latter, however, is not common. Mr. Peach also
mentions the occurrence of porphyry, gneiss, Oolite, Lias, and Chalk-
flints. Mr. Dick told me that fragments of Oolite are not uncommon ;
I myself observed many pieces ‘of it in the drift at the mouth of
Berriedale.

I did not see many large erratic blocks, but Mr. Peach tells me
that some big ones of conglomerate are scattered across the country,
more particularly between Weydale and Stonegun, near Thurso.
He saw very few on the Scarabin hills. Mr. Dick told me he had
not observed any large blocks which might not have been derived

1866. | JAMIESON—CAITHNESS. 267

Fig. 5.—On the Thurso Water, near Thurso.

BE. Stream. Farmhouse. : WwW.

\ i ioe :
E —
\
see - | ay en
Os ef | fee: °
= = /
= 6 . | 0
- 2 | eee &
os 3° ~ x es
Seo: 2 i e*
ie ee ~ o

The high banks on both sides of the stream consist of unstratified pebbly clay
or gritty mud with a few traces of broken shells.

from rocks in some part of the county, with the exception of one of
granite near Castletown, which he thought was different from any
of the Caithness granites, and had probably come from Sutherland,
where a similar quality of rock is known to occur.

4. State of the Shells.—The shells, as a rule, occur in broken frag-
ments. The most common kinds are the Cyprina Islandica, Turri-
tella ungulina, Astarte borealis, A. elliptica, Tellina calcaria, and T.
Balthica. Although broken pieces are the rule, yet exceptions
sometimes occur. Thus, during the search that I myself made, I
found one entire valve of Astarte borealis, another of A. elliptica,
and two small ones of A. compressa, likewise a specimen of Natica
nitida and another of UN. Jslandica, both almost perfect. And in
the collections of Mr. Joseph Anderson and Mr. Robert Dick I saw
several entire single valves of Astarte and Leda, on which there were
occasionally small portions of the epidermis or skin remaining, also
entire specimens of Mangelia and Nassa. Mr. Peach has even got
a specimen of Anomia with both valves compiete, in a fine state of
preservation, and this was in the drift containing the usual assem-
blage of ice-worn stones and broken shells, the only instance of an
entire bivalve that I have heard of. The Turmrtella, which is one of
the most common of all the species, although always more or less
imperfect, yet frequently occurs in large pieces, some of them not
far from being entire. I nowhere observed any instance of the shells
being found in an undisturbed condition, nor could I hear of any
such having been found; there seems to be no such thing as a bed
of laminated silt with shells m situ. LKven the Foraminifera, when
seen through the microscope have a rubbed, worn appearance. No
clay suitable for the manufacture of bricks and tiles or drain-pipes
has been got in Caithnes, it is all too sandy and full of stones. The
laminated brick-clays are, in short, entirely absent.

Many of the shell-fragments show marks of glacial action. It is
generally on the stouter pieces of Cyprina and Astarte that these are .
to be seen, but I found some fragments of Tellina calcaria distinctly
marked. Now this is rather a delicate fragile shell, and the fact of
its being so marked and yet not crushed to powder, shows how gentle,
in some cases, the action must have been that imprinted these
markings. Where the shell-fragments are of an elongated form, the
scratches run lengthways along them, just as they do on the pebbles.
I have one piece of shell, which I picked up myself, not quite an
inch long, most beautifully marked with a multitude of fine parallel
scratches as if done by the point of a needle, and quite polished even

vu 2

268 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Feb. 7
5]

on the broken edges. The fragments of Turritella somehow seldom
show these markings.

5. The Glaciation of the Rocks and Boulders.—One of the objects I
had particularly in view was to note the direction of the glacial
markings on the rocks, and to ascertain whether they could be ac-
counted for by a movement of ice proceeding from the interior of
the country towards the coast. I therefore lost no opportunity of -
noting the bearings of the scratches wherever I saw them. The
result showed a pretty uniform direction over the whole district, the
lines running N.W. and 8.E. Thus :—

At Rea i. np siogse eres toi y. imp niaatoneean toe ts bls che Soipveiiea eee N. 45° to 55° W.
Ditto at another place. attri. mie eae - me cls» eietia eee N. 50° W. ©
About halfway between Forss and Reay ................ N.W.
In the bed of the Forss water .... N, 45° W.
On the top of Leurery hill (about five miles $.W. of Thurso) N. 55° to 60° W.
At Scrabster bar hour’ ti s.04.\. wicca eases deleicuie wicca ee N. 30° W.
On’ the top ofa cliff near Skirza Head mm... 5-2... a -6 oe ie N..65° W.
In the bed of the Freswick stream .........-..:..---0e0e N. 35° to 40° W.
At Kerssvhar bout’ <3... 2.0 c. Blew ceeeoa <i ore oaeice ere eens N. 35° to 40° W.
At the new pier/at Pulteney (Wick) 9.0. 2-520. seme oe N. 15° W.
On the top of the cliff near the old castle of Wick ........ N. 15° W.
Some cross markings here pointing W. 15° S.

In the bed of the Milton Burn (near Wick) .............. N. 43° to 45° W.
In the bed of the Haster Burn (near Wick), in several places
(finely displayed‘. fet satus eit tate Oe a ee ee ee N. 55° W.
On a hill-slope between the streams of Dunbeath and Berrie-

dale, on conglomerate, well marked...................- N. 60. W.
On the roadside, near Berriedale Church ................ N. 60° to 65° W.
Ditto, one mile south of Berriedale inn .................. N. 45° W.
Ditto, two miles south of Berriedale inn ........: . N. 40° W.
On Lumps of conglomerate (having an evident ‘stos-seite on

the N.W.) about two miles south of Berriedale.......... N. 34° to 40° W.

In the above the correction for compass variation has been applied.
Mr. Peach in reference to this subject says, “ All the grooves that I
have met with on the rocks below the clay in Caithness run N. and
S. with deviations to the EK. and W.; I have found them almost all
over the county.’ Upon inquiring of Mr. Peach, I find that his
bearings are by compass. Remembering, therefore, that the com-
pass in that district at present points fully 25° to the west of north,
it will be seen that his account of the matter Bes corresponds
with my own.

The impression left upon me by all I saw was, that the movement
had been from north-west to south-east ; for where I observed any
indication of a Stosseite it was on the north-west side. In order to
obtain further evidence on this point, I endeavoured to trace the
boundary of the dark-grey drift; for I thought that, had the move-
ment come from the north-west, ‘the dark- -grey mud derived from the
Caithness flags should overlap the red grit and conglomerate towards
Dunbeath and Berriedale, while the flags themselves should be over-
lapped at their north-western boundary towards Reay by a different-
coloured drift. This I found to be the case. The dark-grey mud fills
the bed of the Forss water, but does not extend beyond the watershed
between that stream and the Burn of Isauld; and at Reay, the drift

1866. ] JAMIESON——CAITHNESS. 269

covering the grey flags is of a reddish brown colour. On the other
hand, the dark-grey mud stretches south-eastward, past Lybster, into
the bed of the water of Dunbeath, and lies in heavy masses even in the
south branch of that stream. I also traced it to the mouth of Berrie-
dale water, where it mingles with the reddish-brown drift that pre-
vails from there to the Ord; but further up the Berriedale Glen to
the base of the Scarabin hills the colour is reddish brown. The dis-
tribution of the dark-grey mud therefore harmonizes with the suppo-
sition that the transport had been from the north-west ; and a move-
ment of ice from north-west to south-east across Caithness is totally
at variance with the notion of the scratches having been caused by
glacier-action proceeding from the interior of the country towards
the present coast.

I have already mentioned that the stones imbedded in the drift of
Caithness very often show the glacial striae. When examining the
sections along the Haster Burn, in company with Mr. Joseph An- .
derson, I remarked that the striz on the imbedded fragments yene-
rally agreed in direction with those on the rock beneath. The
scratches on the boulders, as usual, run lengthways along the stones
when they are of an elongated form; and the position of these stones,
as they lie imbedded im the drift, is, as a rule, such that their longer
axes point in the same direction as do the scratches on the solid rock
beneath, showing that the same agency that scored the rocks also
ground and pushed along the drift. Interspersed amongst these
ice-worn stones were many fragments of shells—themselves also
scratched—and some univalves almost entire.

This coincidence of direction between the scratches on the stones
and those on the subjacent rock I also observed in the section along
the Milton Burn; and I am inclined to think it is a characteristic
feature, and will be found of general occurrence. In my paper “On
the last Geological changes in Scotland,’ I have described it as a
feature of the boulder-earth or glacial-mud which lies beneath the
marine beds in the midland region of Scotland.. The appearance of
the drift along the Haster Burn and in many other places in Caith-
ness is, in fact, precisely the same as that of the Old Boulder-clay
of the rest of Scotland, except that it is charged with remains of
sea-shells and other marine organisms*. Mr. Anderson told me that

* The glacial drift of Caithness is particularly interesting as an example of a
boulder-clay which, in its mode of accumulation and ice-scratched débris, very’
much resembles that unstratified stony mud which occurs underneath glaciers—
the ‘moraine profonde’ as some have called it. But the presence of marine or-
ganisms, and the direction of the glacial striz, which indicate a movement of ice
from the north-west, where there is now nothing but open sea for an immense
distance, together with the absence of moraines, are all suggestive of marine
conditions having prevailed during the deposition of the Caithness drift. It
would therefore seem that sea-borne ice can in some places accumulate a mass of
unstratified stony mud so like that which is found underneath a glacier as to be
undistinguishable from it, except by containing remains of sea-animals. The
scratched boulders used to be looked upon by some as a certain test of glacier-
action. ‘‘ Ces cailloux,” says Ch. Martins, “sont, pour ainsi dire, /e fossile carac-
‘éristique de la présence d’anciens glaciers.” —Bull. Geol. Soc. of France, 2 ser.
iv. 1191, 1847. In the Caithness drift, however, not only the stones, but the

very sea-shells are glacially scratched, a circumstance which I have also observed
in some of the glacial marine beds cf Aberdeenshire.

270 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 7,

specimens of this drift from the Haster Burn had, upon microscopical
examination, yielded him abundance of Foraminifera and other mi-
nute remains of animal life. Mr. Anderson was the first to apply
the test of washing and microscopic examination to the Caithness
Drift, and Mr. Peach says that all the samples tried from between
John O’Groats and Wick had yielded them in this way more or fewer
Foraminifera, Entomostraca, &e.

6. Absence of Moraines and Gravel-hillocks.—I saw no abrupt
mounds of gravel and boulders in Caithness, nothing like the Kaims
or Esker ridges, nor anything like a moraine. Mr. Dick told me he
had noticed some gravel-hillocks near Dirlet, but nowhere else.
Circumstances prevented me from exploring the neighbourhood of
Morven and the adjoining hills, but in a walk along the Berriedale
Glen, from the base of the Scarabins to the sea, I observed no mo-
raines. ‘This part of the glen is deep, narrow, and winding. There
is a good deal of unstratified reddish-brown stony earth in some
places along the foot of the hills, in which some ice-scratched stones
vccur, and where the mouth of the glen opens upon the sea there is
a great depth of it on the south bank. Large boulders of many
different kinds—granite, sandstone, conglomerate, quartzose mica-
schist—occur here, also fragments of shelly limestone, and bits of
dark sandstone containing lignite. Most of this accumulation of
drift has a reddish-brown colour, but there is also a mixture of
dark bluish-grey stuff, in which after some search I got nine or ten
small pieces of shell and a bit of a Balanus. This drift is like-
wise to be seen on the face of the sea-cliffs on the north side of the
stream.

There is also, so far as I observed, very little valley-gravel ; in-
deed I am inclined to think that the valley-gravel, such as we find
it in the midland region of Scotland, is not developed in Caithness.
That which occurs in the ruts of the various streams is merely what
might be produced by the long-continued action of currents such as
we see flowing in them at present. The gravel in these channels
seems to be merely the stones derived from the banks of drift along
their course, the finer sediment having been washed away by the
current. So far as I saw, these beds of gravel are not extensive, and
are confined to the bottom of the channels in which the streams run.
These watercourses are trenches which appear to have been cut out
of the drift by ordinary river-action.

7. Relation of the Caithness Drift to that of the rest of Scotland.—
Caithness, therefore, differs from the midland region of Scotland i
regard to its glacial phenomena :— ,

Ist. In that the glaciation of its rocks seems to have been pro-
duced by a movement of ice proceeding, not from the interior of the
country, but apparently from an external region to the north-west.

2nd. In its covering of drift, which resembles the Old Boulder-clay
of the middle of Scotland in regard to its physical arrangement, but
differs therefrom in the prevalence of marine organisms scattered
through it.

3rd. In the absence of glacial-marine beds deposited with the

1866. ] JAMIESON——CAITHNESS.. Al:

indications of tranquillity that we observe in the regions further to
the south.

4th. In the deficiency of valley-gravel, and the absence of mo-
raines and gravel-hillocks.

It is very desirable to ascertain the area over which these features
prevail. From what Mr. Peach says of Shetland, I am inclined to
think it will embrace both these islands and the Orkneys. I did
not examine the north coast of Sutherlandshire, and cannot say how
far in that direction the same characters extend; but in passing
rapidly along the east coast of Sutherland and Ross it seemed to me
that there was a change after going south of the Ord of Caithness,
the shelly drift vanishing, while great moraine-like heaps of gravel
make their appearance at the mouths of the several valleys. At
Brora, for example, there is a remarkable assemblage of hillocks
which come down close upon the shore, and at Dornoch Frith I
noticed similar deposits on the north side near Clashmore, and on
the south side along the base of Struie hill. At Muir of Ord, between
Beauly and Dingwall, I examined another fine range of gravel-hil-
locks, extending from the neighbourhood of the railway-station
westward up the flank of the hill to a considerable height. But the
finest of all is a most remarkable series of ridges commencing at a place
ealled Kildrummy, about two miles from Nairn, and ranging south-
westward by the Loch of the Clans and-Loch Flemington towards
Culloden moor, in the neighbourhood of Inverness.

The direction of the glacial scoring in Caithness, if produced south-
eastward, would pass the corner of Aberdeenshire near Fraserburgh ;
and here I may mention that I have recently observed traces of gla-. _
cial action at a few places in the neighbourhood of that town, and
it is interesting to remark that their direction corresponds with that
in Caithness, being N.W. and 8.E., and produced by an agency which
seems to have come from the north-west. Thus :—

On a rock surface newly exposed in a railway-cutting near

Seite ees S02 «ar Pain ya's ¢ «ied s oy «lo ASVahe Wa)» wfBie aos, sees N. 65° W.
At another spot in the same cutting ........ Rieter iene cas > N. 45°. W.
PR GaeEIE SH: QUART: 5 oe cit oie ce clase wre ol lem nie sien wide 6 N. 40° to 65° W.

On the coast at St. Colms, about five miles south-east of Fraser-

burgh, there are some rocks which have a strong appearance

of glaciation and a north-west Stosseite, while long fluted

COT Nie TO CIAT Es 5s ES A a ee IE Eee Mer ce artes N. 65° W.;

but there are no trustworthy scratches.

The rocks also on the south side of Fraserburgh harbour have

an appearance of glaciation coming from the north-west or

west-north-west, and beside the turntable at the railway-

station there are some scratches on the rock in varying

directions.

Again, it is worthy of remark that along the coast from Banff to
Peterhead, the prevailing colour of the glacial clay is dark bluish-
grey, quite like that of Caithness. This, however, may be owing to
the sediment from the clay-slate of Banffshire having drifted east-
ward; but it may also be partly due to a drift of fine muddy matter.
from Caithness. The dark bluish-grey clay ranges south to Peter-.
head, where it thins out and is interstratified with the red clay.

272 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 7,

which prevails thence all along the east coast as far south as Fife-
shire. In the neighbourhood of Peterhead, as for example, at the
Invernettie brickwork (See Quart. Journ. Geol. Soc. vol. xiv. p. 518,
1858), there are many boulders of red and grey sandstone, and also
of a tough greenish-coloured stone, all of which resemble rocks that
occur in Caithness, but, so far as I know, not in the adjoining parts
of Aberdeenshire. I have always been at a loss to account for these
boulders near Peterhead, and also for the dark-grey tint of the clay
between that town and Fraserburgh, seeing that the rocks of the
district consist of mica-slate and granite. But looking at the direc-
tion of the glacial markings, [ am somewhat inclined to think that
both the boulders and the dark muddy sediment in this low projecting
corner of Aberdeenshire may have drifted from Caithness.

8. Place of the Caithness Drift in the history of the Glacial period.
—TI have now te consider the relation in time of the glacial pheno-
mena I have been describing to those of the rest of Scotland. In
the parts of Caithness which I examined, it seems to me that we
have only one glacial deposit, and I am further of opinion that we
cannot separate, in point of time, the period of its accumulation and
present arrangement from that of the scratching of the rocks on
which it lies: for the coincidence in direction of the scores on the
rocks with those on the stones imbedded in the drift shows that it
was one great movement—long-continued probably—that marked
the rocks and carried along the mass of stony mud that now rests
upon them; in fact it was the movement of the drift across the
surface of the rocks that scratched them. Now in the midland
~ region of Scotland we have evidence of three well-marked stages in
the Glacial period—Ilst, the great glaciation of the surface and
deposition of the Old Boulder-clay or till; 2nd, the finely laminated
glacial-marine beds; 3rd, the overlying gravels and moraines. To
which of the divisions represented by these three are we to refer the
Caithness drift? or is it the equivalent of any two of them, or of all
the three ? . | ;

The Caithness Drift contains remains of sea-shells all through it,
often from top to bottom, and these shells are broken, rubbed, and
scratched, evidently by the same agency that marked the rocks and
boulders. This is an important fact, for it gives us a date for the
action. The scratching and breaking of the shells was an event at
least as late as the time when the Mollusca lived that formed the
shells; and, seeing that the shells extend to the bottom of all the
sections of the drift, it is further evident that none of it was lodged
in its present position at a more remote date. Indeed, it is in the
lower part of the sections that the fragments of shells chiefly occur ;
in some cases, as for example at Wick and Keiss, they are scarcely
to be found in the upper portion. If, then, we could find the date
of the shells, we should have a clue to the age of the drift: itself.
In the midland region of Scotland the Old Boulder-clay, and the
scratching of the ice-worn surface of rock on which it rests, evidently
preceded the time when the mollusca lived whose remains we find
in the marine beds above it. At Loch Gilphead, in Argyleshire,

1866. | JAMIESON—CAITHNESS. 273

rows of Mya Uddevallensis, entire in their burrows, are found in
the fine marine sediment overlying the Boulder-clay, and many
other facts of a like nature might be cited. Now if the Caithness
Drift is the equivalent of the Old Boulder-clay of the rest of Scot-
land, why do we not find some fine laminated clay above it, as we do
in other places ? é

It may be said that the mollusca of the Caithness Drift are an
older group than those found in the marine clays of the other parts
of Scotland, and therefore, although these mollusca lived during the
Caithness Drift, it does not necessarily follow that the latter deposit
is more recent than the Old Boulder-clay of the rest of Scotland.
An inspection, however, of the list given in the Appendix to this
paper does not suggest an older age, but the contrary. In order to
place this in a clearer light I have drawn up Table 2, in which
the geographical relations of the Caithness shells may be compared
with those of groups from the glacial beds of other parts of Scotland.
Thanks to the efforts of Mr. Peach, we have a very good list from
Caithness; moreover, the specimens have been all examined and
named by Mr. Jeffreys, an eminent authority in these matters, so
that the list may be used with all confidence.

I think it is a fair inference that the more nearly a group of
British fossil mollusca resembles the assemblage of species now living
upon the shores of Britain the more recent is the period to which
that group belongs. I have accordingly ranged the groups in a
series, those which show the lowest percentage of British forms
being reckoned oldest. From this Table it will be seen that the
Caithness group is the most modern, except that of Fort William,
which in a former paper I had referred to the very close of the
Glacial-marine period (Quart. Journ. Geol. Soc. vol. xxi. p.174, 1865),
while the proportion of Arctic species is less at Caithness than at
any of the other localities—less even than at Fort William. It is
not pretended that all these groups represent distinct stages in the
Glacial period; several of them I have no doubt were contempora-
neous, but I think we are entitled to suppose that the Errol, Elie,
and other groups at the beginning of the list are older than the
Caithness and Fort. William ones. Here, then, we have further
evidence to show that the accumulation, or at least the final arrange-
ment, of the Caithness Drift was a comparatively late affair; it
therefore ought not to be confounded with the Old Boulder-clay.
It seems to me that it ought to be referred to the Glacial-marine
period. A set of marine beds containing Arctic shells were probably
deposited over the low part of Caithness; and much drifting ice
seems to have passed over the district from the north-west, which
crushed and destroyed these marine beds, broke the shells, and mixed
them up with other superficial débris into that mass of rough pebbly
mud which now overspreads the surface. These marine beds were
probably of different ages, the older containing Arctic species, the
later containing chiefly Boreal and southern forms. This would
account for that mixture of species which we observe in the Caith-
ness list.

274 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 7,

At Invernettie, near Peterhead (see Quart. Journ. Geol. Soc. vol.
xiv. p. 518, 1858), the base of the section shows fine stratified clay
and sand free from stones, above which there is a thick mass of
rough pebbly clay like that of Caithness, containing well-scratched
boulders of granite, sandstone, d&c., with some broken sea-shells,
which also show traces of glacial scratching. Here, then, we have
a mass of unstratified drift closely resembling that of Caithness,
and from its position above the fine laminated clay apparently later
than at least a part of the glacial-marine beds.

But the glacial deposits at King-Edward, in Aberdeenshire, throw
still more light upon the relations of the Caithness beds. Some
sections recently laid open there have enabled me to understand
their arrangement far better than formerly. At this locality there
are deep masses of unstratified pebbly mud of a dark-grey colour,
very hard and firm, containing stones (some of which are ice-worn
and striated) and fragments of shells, which are likewise occasionally
scratched. It is, in short, so like the Caithness Drift in every re-
spect—in colour, texture, and organic contents—that I can perceive
no difference between them. It has been called “‘ the Boulder-clay”
by Mr. Robert Chambers, who visited the locality in 1855*. Besides
this coarse stony mud there are some beds of fine stratified sand,
which often contain remains of shells in considerable abundance,
most of them broken, but many of them entire. The bivalves
always occur in detached pieces and want the epidermis, as if they
had been washed about by water. ‘This, I believe, is the bed that
yielded Hugh Miller’s specimens, and from which I have obtained
most of the species enumerated from King-Edward in my paper on
the last geological changes in Scotland. But there is another bed
of fine dark-grey silt, free from stones, containing Arctic shells en-
tire, and apparently in situ, with the epidermis on. The Tellina
calcaria occurs here of large size, with both valves connected by the
ligament and shut, also Leda, Natica, and others; they are very
sparingly dispersed in the silt, which contains streaks of black car-
bonaceous matter, proceeding probably from the decay of seaweed.

It also contains Foraminifera. This bed of silt I noticed in 1857 ;

Fig. 6.—Section at King-Edward, Aberdeenshire.
N

1. Valley-gravel.

2. Pebbly clay.

3. Fine sand with shells.

4. Fine silt with shells 2 sztu.

5. Rock.

* See ‘ Proceedings of Royal Society of Edinburgh,’ Dee. 17, 1855.

1866. ] JAMIESON—CAITHNESS. 275.

but, owing to the want of good sections, the arrangement of these
- various deposits was then obscure. It is, however, as follows :—

Commencing at the surface we have— iingeknenp
in feet.

1st. Water-worn gravel and sand, stratified, often rather coarse and

pebbly, and somewhat ferruginous. Contains no fossils, so far

PPP MMRRE NEN SCOM he as oss eee alata. sacs set ds od cae vas bo eeges 10 to 25
2nd. Unstratified pebbly mud of a dark-grey tint, hard, and diffi-

cult to pierce. The stones in it are of small size, but numerous,

and some of them glacially scratched. In the upper part I

could see no shells; but shell-fragments occur in the lower part,

increasing in numbers towards the base. Some of the shell-

fragments show distinct traces of glacial action ............
3rd. Fine brownish sand, in some places rich in shells. This sand

is interstratified with the upper part of the subjacent bed ...... lto 2
4th. Fine dark-grey silt, free from stones, containing Arctic shells

complete, and apparently in situ; they are, however, mostly

decayed and somewhat crushed, so that it is difficult to extract

them. This silt is very firm, as if much compressed, and the

greater proportion of it consists of fine muddy sand. The base

of this bed has not been exposed, but it has been excavated by

Mr. James Runciman (who was so good as to lay it open at my

request) to a depth of 10 feet. No difference in the quality is

to be seen to this depth; no stones. The upper surface of this

silt is about 150 feet above the sea.

20 to 30

Here, then, we have a thick mass of drift, exactly like that of
Caithness, clearly overlying a glacial-marine silt, with shells zn sztu.
The broken shells in this coarse upper drift seem to have been derived
from the beds below. In one part of the bank I found, at the bot-
tom of the coarse pebbly mud, beds of fine silt with broken shells
and confused stratification; these seemed to be ordinary marine
beds disturbed from their original position by the agency that lodged
the overlying drift. Where this disturbing action was so great as to
completely break up and destroy the fine silty layers then we should
have sections like those of Caithness, where the mass is unstratified
from top to bottom, and I believe in many places of the King-Edward
banks this will be found to be the case. Large boulders are rare in
the King-Edward district, but I saw one of Greywacke from 3 to
4 feet in length, which seemed to have dropped out of the coarse
pebbly mud. |

Fig. 7.—Section across King-Edward valley.
N. Stream. s.

A. Greywacke and clay-slate,
B. Glacial deposits.

In a notice of these King-Edward (the name is a corruption of
Kinedart) beds in the 14th vol. of the Quart. Journ. Geol. Soc. 1858,
p- 525, I remarked that the shells in the fine silt were often crushed
in a remarkable way, as if by sudden pressure from above.

276 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. | Feie7s
e

The glacial beds of the south of Arran (first described by the Rev.
It. B. Watson, and more recently explored by Dr. Bryce and the Rev.
H. W. Crosskey) seem to have many points of resemblance to those
of King-Kdward. There are beds of fine clay containing Arctic
shells, sometimes in a broken or crushed state, but occasionally en—
tire and apparently an situ. This fossiliferous stratum is covered
by a great thickness of what Mr. Watson calls “ Boulder-clay,” but
which Messrs. Bryce and Crosskey term “ Upper Drift beds.” If I
understand Mr. Watson rightly, this upper stuff occasionally contains
broken shells. The fine fossiliferous clay sometimes rests immedia-
tely on the older rocks, at other times, according to Messrs. Bryce
and Crosskey, there is a mass of clay beneath it of harder, coarser
texture than what lies above, and containing stones and boulders on
which glacial action is more apparent, and they would restrict the
term ‘‘ boulder-clay”’ solely to this lower stuff. Mr. Watson mentions
the occurrence of glacial beds beneath the fine shelly clay, but, ac-
cording to him, they vary a good deal in character, and he does not
draw the same strict distinction between them and the upper beds.

If want of stratification, hardness of texture, and abundance of
well-glaciated stones and boulders are to be the tests for what we
should call genuine Boulder-clay, then much of the Caithness Drift
will stand the ordeal, and, moreover, the shells are as well glaciated
as the boulders. ‘The upper pebbly mud of King-Edward is also
often very hard and firm.

If the Old Boulder-clay or till has been produced, not in the sea
but by glacier-ice moving on the land, it ought to be devoid of
marine fossils. What we now want is a microscopic examination of
our various so-called Boulder-clays. Messrs. Anderson and Peach
have made a commencement with those of Caithness, and find them
full of minute organisms. This was to be expected from the presence
of the sea-shells. The Boulder-clay, however, which hes beneath
the beds of Arctic shells in the midland region of Scotland is remark-
able for the absence of fossils, but it yet remains to be seen how it
will stand the test of washing and microscopic examination.

9. The post-Glacial period in Caithness.—So far as I observed, the
post-glacial conditions in Caithness do not appear to have differed
much from those in the rest of Scotland. Some indications of a
submerged forest, or old land-surface, occur at Sinclair Bay. The
peat bed, close upon the shore at Ackergill, contains clusters of seeds
of land-plants and also some remains of trees or bushes. Mr.
Cleghorn, of Wick, thinks this peat bed is a marine deposit of matter
carried into the sea by the rivers. After examining it in company
with him I am inclined to differ from this opinion. The peat is
covered by a mass of blown sand, which has insinuated itself into
some of the crevices and openings of the peat, but I saw nothing to
induce me to believe that there was any interstratification, of peaty
matter with marine sediment.

Mr. Dick told me that at Thurso some peat, containing haveloumes
and twigs, had been got near the beach on the west side of the
town, but I could not learn whether it was 7m situ or transported.

1866. ] JAMIESON—CAITHNESS. | 277

There are some traces of a recent change in the relative level of
sea and land along the coast, but only to a very slight extent. The
elevation of beds of coast-shingle cannot be depended on with much
exactitude as evidence of the former level of the sea, for storm-waves
fling up banks of pebbles to various heights, according to the nature
of the coast. Even large boulders and great heavy blocks are moved
in this way far above the reach of the tide in calm weather. A re-
markable instance of this may be seen a little to the south of Wick,
which has been cited by some as an example of iceberg-action. But
I was assured by Mr. Joseph Anderson that within the last four or
five years some of these blocks have been tossed about by the great
waves which occasionally break upon the coast during severe gales,
a statement which is confirmed by the observations of Mr. Peach.
Mr. Cleghorn also told me that he had seen blocks of thirty tons’ weight
turned over by the surf 15 or 20 feet above the present level of the
sea. Beds of estuarine silt, that have been accumulated in well-shel-
tered positions, afford a better means of determining the former sea-
level. There are, however, no estuaries in Caithness, and I therefore
cannot speak with confidence as to the amount of this recent change
of level, but from all I saw I should think the present position of the
land is only a very few feet higher than formerly. The beds of old
estuarine mud at the firths of Dornoch, Cromarty, and Beauly attain
no great height above the present sea-level—not so much as in the
firths of Tay and Forth, or even at the Montrose basin.

Later than this last rise, as shown by their position, are two
ancient tumuli in Sinclair Bay, known as “the Burkle Hills ;”’ they
are of large size and of a bee-hive form. They seem to contain some
internal chambers, or stone structures of some sort, but have not been
properly explored. One of them was partially opened last year by
Mr. Laing. The bases of both are only a few feet above the present
reach of spring tides; one of them, at least, is not more than 4 or
5 feet above it. The fact of these old remains being later than the
raised beach agrees with my observations at the Estuary of the
Ythan, in Aberdeenshire.

Kjokken-moddings, or heaps of edible shells mixed with burnt
stones and the teeth and bones of various animals, abound along all
the sandy bays of Caithness; I observed them in great numbers at
Reay, at Freswick, and at Sinclair Bay. They are often covered by
a considerable thickness of blown sand. At Reay I noticed a great
quantity of the shells of Helia nemoralis in these heaps, as if it had
been eaten there along with the limpets and periwinkles. Several
teeth which I picked up from these heaps were examined by Dr.
Turner, Demonstrator of Anatomy in the University of Edinburgh,
who pronounced them to belong to the Pig, Horse, Ox, Deer, and
Sheep.

APPENDIX.

In regard to the following Tables I have again to acknowledge
the kind assistance of Mr. Jeffreys, who has done me the favour of
revising the Caithness list, as well as the lists from which the abs-
tract, Table no. 2, has been prepared.

278 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

The list of Caithness shells combines Mr. Peach’s two lists (for
which see ‘ Brit. Assoc. Report’ for 1862, Trans. of the Sections, p. 83,

ibid. for 1864, p. 61), and also some additional species enumerated

in a paper lately communicated by him to the Physical Society of
Edinburgh. | !

For the Fort William list see Jeffreys in the ‘ Brit. Assoc. Report’
for 1862, Trans. of the Sections, p. 73. For that from Elie see the
Rev. Thomas Brown in the ‘ Proceedings of the Royal Society of
Edinburgh’ for March 2nd, 1863. The others will be found in the
Appendix to my paper in the ‘Quart. Journ. Geol. Soc.’ vol. xxi.
p. 161, 1865.

In the two following Tables

Southern means species living on the west coast of Europe, to the south of
lat. 50°.

British means species living on the coasts of Britain.

Northern means species living on the west coast of Europe, south of lat. 60°
and the Arctic circle.

Arctic means species living within the Arctic circle.

NN. H. American means species living on the east coast of North America.

TasiE 1.—List of Mollusca whose Shells are found in the Glacial
Drift of Carthness.

|
&
cj di 2
No. 8 4 3 sia
B/2/8/5/A
i) = ° o .
a2;/Al/AIA1A
1 | Anomia ephippium, var. squamula .............. * | oF | oe | | x
2'| Aporshais pesspeletamil) iiiq. o./2 5.2 ceo. ete rele oe 1 | oe |
3 | Astarte borealis=A. arctica, of Forbes & Hanley ere cs |
4 COTM ho eet eters isa. e wh averssnede Suan canst: Oh Due {|e | * | x
Or pS SUCALA ak ot cok a tie os ie apace Soe lau emake eee Coes) ce |
6 suleata;) varvelliptiCay 2 seul. a... alee ee ee cs joe
7 \ Buccimam tnidatimas Ain Ss oe ee Se e |e lel x
8 -| Cardium echinatum™ 22. 52 600. bss oe sonable a * | * | we | oe [ox
9 Cc Iie MOOR RON Ao ee USE cums, Ae b we |e |e | x
10 exiguum=C. pygmeeum, Fd: A... 52.) | ee
11 fASCIALGMN Tan A eae ok ohn che aie aca enee e | ¥ |e | #
12 Grosmlandieumie et > 5k oes 2 es cere oo | is | ae Sen
13 NOE Vex ne mma veut at) ic, 2 eb ARON aren crea aan ge 2k) i eed
14 | Cerithiopsis costulata=Turritella? costulata, Moller; ..| * | * | * | *
15 wicClaiton cinereus. s\ eaea see qari co eee eee % | ok | |e | x
IG Crenella:decussata 7. (oats ae aie eee yo. | # |e | xe |
VS Cy prinaislanclicay. ct. ttn ss tees ee eer eee x |e |e |e | x
18 | Cyrtodaria (Glycimeris) siliqua ................ ws (besods lege eee ee
LO Dentaliumrabyssormmit: att. apie as aceon eee cee be * | ok |
20 SMUD AMIS, saassans tore vo feetahoruotee eae anata eer eee 6], Fy] ol eee
21 | Donax vittatus=D. anatinus, F.& H............. * |e | * | x
22s AsusvamM HGS He CsA gee wee ec ce a e a cleo ee 2] % |e | x
23 | Lacuna divaricata=L. vincta, Ff. & H............. x | *¥ |e |e | x
24 | Leda minuta=L. caudata, F.& H. .............. ws | 3 | Ge ee
25 pernula, var. buceata 4.00025 2.0. 08. Sik .. |. + | alee
26 POS MNGea aPstises saeresth “hate Nene Saas eeels oe). 5 Pie |e |e] x
27, | Laktton iad ton ea ie cea ack farmer Seah ase ese pe = x | ¥ |e | x | x

1866. | JAMIESON—CAITHNESS.

Tasxe I. (continued).

279

No.

E
3
=
w
Littorina obtusata=L. littoralis, PF. wee VTE tials, os oak *
Lucina borealis ...... smo ye ioe
spinifera .. UPR RE reen mete Grob rine Re Oe
PUP ANAOING A ops 2 she eats ee aie aie,e onic. o tune siars apse he *
Mangelia levigata=M. nebula, F. f H...........] ¥
GSR se Sek an ctots crore chalatd Suvaahe calle’ Sale *
—— pyramidalis .......... aici Me ini stagaan Tasdoilh dis
Pie EAIEE o) ane. he. « >: im) wish sy si ws seit, oye wie scoraysioreava| yam
PIG EUR ache seh age- are, Ialedas Tae!) singe wage, sien wee, ci sis *
MIE MERCHEM CNS ST orn cee aes laces Sas adele ae aid on *
“vars Waddevallonsis’. 600.5 JS iil. eee. ce
PBT CNCM A =, 5°, < cyevaljele acscua(gupia Siniietd Lhsiwtala yale, fs *
modiolus= Modiola modiolus, F. & H. .....
ONS) UTICKASSATA «ose. cos we emt t a cece es eens *
Natica affinis=N. clausa, Brod. ¢ Sow. . Roatan ee
Islandica=N. helicoides, F. & H. .......... 2
PMU LR eR ceric telat avelcharel ns eis were ses aseisereis 6 dye oe > *
pallida= N. Greenlandica=N. pusilla, F. & H.| ..
SURE CL Mma aler Santee eG ny waic's, fe, Syeteixhare, #1 2 0 ae *
ISS ECULE) 0 el eT ee x
sulcata=N. decussata, F. & A.) .........60. *
Odostomia acicula = Eulimella acicula, F. & H.....| *
albella (see F. & H. vol. iii. p. 286) ........| ¥
Pn PPE CHS EL aya) a/8\ «acces tac aietr «coat x's, 4-atacete of oad ws *
Sper ia WUGRER oc. fis sie alse das Pela aiode a Ws. ae *
Roce mS ITENIGUIS a Tis. sine dts ssi delarefote ve wale ie
IRANIAN ets’ A estas. ayjeledeseks) oheiais' steal ols la aie chee *
SCH CULALIS | ss a Cadelsely cleleia = oa «2 eletalas eecemuvlc *
PeUMIsOUTa LAPIS =, so cin 26. ssn n ot 3 © Sisigc We we sic *
ihyrenonella psittacea ... 1.5 22s ce ce cee ce een ce
Rissoa parva, var. interrupta ........00cee. eee %
Saxicava Norvegica=Panopza norvegica, f. & H...| ..
TUFOSAs) | Laree: LORIN. is, 5 6 a slajnie pivinv@ ao) Sidini nce oe
Ne@lcenEbus CanGIGUs ©. 2... 2 ce sae ws cis siete ve stele %
Tellina calearia=T. proxima,-/. & 7. ......:.... -.
—— Balthica=T. solidula, /. gf H. ......... Psi
Monmeatellafaseiatar ss Jo. fi ceases ae ee weal eee *
Trochus Groenlandicus=T. ee UBS SeMEAT x ail ze
Eee PEUUEY ER. 5, biedavsyarey deis\elcloys See reli oiej aya) eeig ples acti
= AZ IITINUIS, “ofa < 3) ole sinisl. mages 46) Aen a's, Se waljeswaie *
Trophon clathratus=Fusus scalariformis, Gould ..| ..
Savas COMMER Ai. oe tetris lc" esas ote sell»
truncatus =. elathratuss if G? A: pecs |.
Turritella ungulina=T. communis, DPS ELAS oi Pegs *
OPTDUIS) CISTI OO gaan ee ony ARP Re on no *
Gatlina—=,V strichula, BO lle. .wercwinw ones ap *
—— lincta= Artemis lincta, Ff. & H. ..........- .| %
vomess GUE SAI SE IC Ste Rec e CSS S56 9. ci) elo Noa CIcIQHSE *
46

=per cent. .. ae 61

rs
8
3 5
al il le
Alal 4] 2
eu] PECs
* * %
* * *
* *¥ *
*
¥
ale ¥* * *
* * *
* * x *
* * * *
atte 0 * *
* * * *
* * * %
* * * *
a5 * * *
* * * *
x | * | x
* * * *
¥
* *¥ *
¥* *
* *
(* *
* * So *
* * *
45 * * *
¥ ¥*
* * *
* * * ¥*
Seulbe a se aioe
* * *
* * +* *
exe a4 * *
*
oie * x *
* * 4 | ¥
* * *
* | * * *
pe ios % *
a
At * * %
ntl * ¥ *
* %* * *
* ¥ +
* ¥*
¥ * *
* *
* * *
60 | 66 | 63 | 41
30 88 84 top

280 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 7,

Of the above shells the Turritella and Cyprina are probably the
most common. <Astarte, Natica, Tellina, Sawicava, and Mya are also
pretty frequent, and so likewise are Dentalium entalis, Leda pernula,
Cardium echinatum, and Mangelia turricula. The scale of frequency, -
however, differs in different localities. Some of the species have
been determined from single fragments, as, for example, Venus ovata
and Trochus zizyphinus.

Patella vulgata is a shell I have never myself found in any of our
Scotch glacial beds, but Mr. Peach informs me he got one pretty
perfect specimen, besides two or three fragments. Mr. Dick also
told me he had found it. In regard to some of the other species
Mr. Peach has supplied me with the following information :—“ Pecten
maximus and opercularis, in fragments, occur frequently. Cardium
Norvegicum, two or three hinge-pieces. Husus antiquus, two pillar-
lips. Ostrea edulis, one pretty large shell and several fragments”
and he says there can be no doubt whatever that these occur in the
very same deposits as the more Arctic forms.

Taste II.—Showing the Geographical relations of groups of Mollusca
whose Shells occur in some of the Scottish Glacial beds.

Localities............ Errol. | Elie. ; ae a Paisley.| Kilchattan.|Gamrie.| Caithness. 4 Wilton.
Total number }
of species at j 13 | 14 27 26 16 25 () 47
each locality
rea a ae 58° | 50 | Bean 5B
British, ,,..|.98 | 43 59 61 6O.5 72 80 85
Northern, ,, ..| 62 | 57 93 100 | . 100 96 88 96
Arctic, 5 --| LOO | 100 100 100 100 100 84 89°
| N.E.Ame- 3
ce wa i} 100 | 100 89 85 87 88 | 55 70

Some interesting information may be gathered from the foregoing
Table.

The Errol and Elie groups, it will be seen, are intensely Arctic ;
the shells are just such as we might find in the sea of Spitzbergen at
the present day, many of the species not ranging south of the Arctic
circle. In them the proportion of British species is less than 50 per
cent., while that of the Southern has dwindled down to a very small
fraction. These two groups I take to represent an early stage of the
glacial-marine beds when the rigour of the climate was at its height.

The groups from King-Edward, Paisley, Kilchattan, and Gamrie
probably belong to a somewhat later stage, for although the general
character is still Arctic, yet it is less strictly so than in the two pre-
ceding. The proportion of Southern forms is far greater, and the
British exceed 50 per cent.

The Fort Wiliam group is probably the latest of all; it is no
longer Arctic but Northern, and the British species exceed ae per
cent.

1866. | GUPPY—JAMAICAN MOLLUSCA. 281

The Caithness group seems to be a mixture of species from glacial
beds of both earlier and later date.

The high percentage of North American forms in all the groups,
but more especially im the first six, is a feature of much interest.

rs

AiRy
iy

Pi ; February 21, 1866.

~ William Henry Corfield, Esq., B.A., Fellow of Pembroke College,
Oxford, University College Hospital, Gower Street, W.C.; Henry
Lee, Esq., The Waldrons, Croydon; Henry Skiffington Poole, Esq.,
B.A., Cape Breton, Nova Scotia; Alexander Ramsay, jun., Esq.,
45 Norland Square, Notting Hill, W.; Charles Pearce Serscold,
Ksq., Taplow Hill, and 24 Oxford Square; George Suche, Esq., 77
Grosvenor Street, W.; and James Maurice Wilson, Esq., M.A.,
Fellow of St. John’s College, Cambridge, Rugby School, were elected
Fellows.

i

The following communications were read :—

1. On the Tertiary Moxttusca of JaMArca.
By R. J. Lecumerr Gurry, Esq., Civil Service, Trinidad.

(Communicated by Henry Woodward, Esq., F.G.S., F.Z.S.)
[Puares XVI.-XVIIL.]
§1. Tue Rerationsures or THE Miocene oF JAMAICA.

In 1862 Mr. Lucas Barrett, Director of the Geological Survey of the
West Indies, brought over from Jamaica and deposited in the British
Museum a collection of Miocene fossils. In 1863 Mr. Carrick Moore
communicated to the Geological Society the results of his examina-
tion of the shells, Dr. Duncan described the corals, and Prof. Rupert
Jones gave an account of the Foraminifera *. In 1864 Dr. Duncan
and Mr. Wall gave a sketch of the geology of a part of Jamaica,
showing the relations of the Cretaceous and Tertiary formations ex-
posed in that island+. In the same communication Dr. Duncan
described several new and interesting corals from the Cretaceous,
_ Eocene, and Miocene strata ; but beyond the general results given in
Mr. Carrick Moore’s paper above referred to, the shells have remained
untouched. It was, I believe, the intention of Mr. Barrett to have
worked out this portion of the subject, and, indeed, he had already had
one plate engraved, which has since been destroyed for want of in-
structions; but as his untimely and lamented death has intervened
to prevent our receiving the benefit of his illustration of the fossils
alluded to, I have undertaken to furnish an account of these remains f.
* Quart. Journ. Geol. Soc., vol xix. p. 510.
t Lbid., vol. xxi. p. 1.
t The following extract from a letter of Mr. Barrett was published by Dr.

Woodward in an obituary notice of that naturalist: “The Tertiary system of
| VOL, XXII.—PART I. =

282 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 21,

In the paper by Dr. Duncan and Mr. Wall, before cited, the rela-
tions of the various strata are so well and succinctly described, that
it is unnecessary for me to do more in this place than to allude to
the fact that the formation whence the mollusca to be described were
derived consists of shales, sands, and marls exposed in several parts
of Jamaica, and that it has suffered great disturbanee, in common
with the Tertiary strata of other parts of the West Indies, and is
frequently found in a position approaching to the vertical. The
identity of many of the species found in these rocks with forms from
San Domingo, Cuba, Cumana, Antigua, Anguilla, and Trinidad, shows
the very extended development of Miocene formations i in the Caribean
area. The period appears to have been one of exuberant develop-
ment of marine life, and the conditions seem on the whole to have
been favourable to the preservation of the shells and other.remains.

The general remarks made by Mr. Carrick Moore in his papers on
the San Domingan Tertiary fossils * are as a rule applicable to those
of Jamaica; and many of those observations have been confirmed by
Dr. Duncan’s investigations of the corals, and those of Prof. Rupert
Jones of the Rhizopoda. Among the new facts brought to light is
the very remarkable resemblance of a portion of the West Indian
Miocene fauna to that of the Maltese beds.

The great difference between the Miocene faunas of the American
and Caribean areas is particularly remarkable when we take into
consideration the alliances of the latter with the European Mid-ter-
tiaries, and the more we investigate the subject, the more we find to
confirm the conclusions already arrived at on this head. Still, there
is a certain amount of resemblance, and, upon examination, I find
that the Petaloconchus Domingensis of Sowerby, appears identical with
P. sculpturatus of Lea, from the Miocene of Virginia.

From my examination of the Jamaican fossils, I am of opinion
that, with the Middle Tertiary beds of San Domingo and Cuba, those
of Cumana, and the Caroni series in Trinidad, the Miocene of Jamaica
is to be considered as representing the upper or later part of the
West Indian Miocene as at present known; while the Chert-forma-
tion in Antigua, the Anguilla beds, and the beds exposed at San
Fernando in Trinidad, belong to the lower and older part of the
Miocene.

In Jamaica the Miocene strata consist of highly imclined marls
and shales, which are especially characterized by Conus, Strombz,
and large Pleurotome, with small Nwmmuline and Orbitoides, as well
as corals. At Cumana we have a fauna almost identical with that
of Jamaica, including similar foraminifera and corals; among the
latter is Flabellum exaratum, Dune. The beds consist in part of

Jamaica is very interesting, though I have not been able to separate it into Sir
Charles Lyell’s divisions. I must first study the recent shells of Jamaica. The
newer Tertiary strata contain a Terebratula (with a short loop) a Terebratulina
(like caput-serpentis) and an Argiope. There is a marl-bed, probably formed in
the deep sea, containing abundance of Pteropods (Cleodora, Creseis, Cuvierta).”
— Ces February 1, 1863.
* Quart. Journ. Geol. Soe. vol. vi. p. 39, and vol. ix. p. 129.

1866.] GUPPY—JAMAICAN MOLLUSCA. 283

sands, with a calcareous conglomerate, which latter yields the coral
alluded to. The Caroni series in Trinidad consists of shales, clays
and sands, and some marls, which are characterized by large Ostree
(O. Haitensis, Sow.). In Cuba the formation consists apparently of
strata resembling those of Anguilla, in which the shells are found
chiefly as casts, most of which have been referred by d’Orbigny to
existing species, but which in all probability will be found to be iden-
tical for the most part with the extinct species found in Jamaica and
San Domingo. Tellina biplicata, Conrad, related to T. ephippiwm of
the Indian seas, and to 7’. Sobralensis, Sharp, of the Portuguese Ter-
tiaries, and WNatica phasianelloides, VOrb., the Tellina occurring in
the Caroni series in Trinidad, and also in San Domingo, and the Na-
tica in Jamaica, San Domingo, Anguilla, and at San Fernando in
Trinidad, are recorded by d’Orbigny from the Cuba beds. The Chert-
formation of Antigua has been fully remarked upon by Dr. Duncan*,
who correlates it with the Lower Limestone of Malta. The Miocene
of Anguilla is a light-coloured marly limestone containing nume-
rous mollusca, chiefly as casts. Among the better-preserved shells
are Solarium quadriseriatun, Sow., snd Natica phasianellordes, d’Orb.
The Echinoderms in this deposit are in better condition, and exhibit
a strong resemblance to those found in the Miocene beds of Malta.
Among the species which are specifically identical, we have Schizaster
Scille, and Cidaris Melitensis, occurring in association with an ex-
tinct species of Echinolampas, only to be distinguished critically from
EL. hemisphericus, and another almost as near to L. scutiforms. Cly-
peaster ellipticus, Michelin, and three living species of Echinoderms
also occur in these beds. At San Fernando, in Trinidad, we have a
numerous succession of gypseous marls, shales, and some partial lime-
stones, enclosing Natica phasianelloides, Orbitoides Mantelli, Num-
mulina, and Echinolampas ovwm-serpentis, as well as some Terebra-
tule.

It must be understood that while there remains but little doubt
as to the very close proximity in age of the Miocene formations of
Cumana, Jamaica, and San Domingo, our information is not quite so
exact with respect to those of Cuba, Anguilla, and Trinidad, owing
to the bad state of preservation of the fossils at the latter localities.
And in endeavouring to correlate these beds, I have used the terms
Upper and Lower Miocene, not as implying that these formatious are
respectively equivalent to the Upper and Lower Miocene of Europe,
but merely as marking what seems to be the relative antiquity of the
Middle Tertiary beds of the Caribean area.

The connexion between the formations found in all the localities
mentioned could only be shown by a general table, including all the
known species from those localities. On the present occasion my re-
marks must necessarily be confined to the Jamaican fossils.

As yet I only know of one species common to Jamaica and Cuba
(Watica phasianelloides) and only two common to Jamaica, Anguilla,
and the Caroni beds in Trinidad. Mr.G. P. Wall, F.G.S8., has kindly
favoured me with a small collection of Tertiary fossils from Cumana,

* Geol. Mag. 1864, vol. i. p. 97.
x 2

284 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. { Fehv2n,

and among these I find fourteen species common to Jamaica. There
are thirty-four species common to Jamaica and San Domingo; and
if the Haitian species not found in Jamaica were now under consi-
deration, the intimate relationship of all the Caribean Miocene beds
would be clearly shown.

Thirteen species have been identified with living forms out of the
total of sixty-one species which are described in this communication.
This would give a proportion of about twenty-one per cent., a some-
what larger proportion than was arrived at by Mr. Carrick Moore
for the San Domingo fossils. Yet I cannot lay much stress upon
the exact ratio of recent species in considering the relative age of the
Jamaica and San Domingo beds; for we have seen that thirty-four
Species are common to both localities, and out of these, seven are
existing species, many of which are widely distributed and have been
found in the Miocene of other localities. Such are Lwcina Pennsyl-
vanca and Venus paphia, which both occur in the Miocene of Europe.
Moreover some of the species identified with living forms do not now
inhabit the West Indies. Among these are Pectunculus pennaceus
and Natica mammillaris. There are several shells in the Jamaica col-
lection which are too imperfect for specific determination, the generic
names of which are given in Mr. Carrick Moore’s paper on these
fossils. .Among them is a small Ancillaria, a genus which | is now
extinct, or nearly so, in the West Indies.

The most characteristic fossils of the West Indian Miocene appear
to be Natica phasianellorides, Solarium quadriseriatum, and Orbi-
toides Mantel, these species having been found in nearly all the
Miocene localities, exclusive of Cumana; and they will doubtless be
ultimately found there also.

The eastern affinities of the West Indian Miocene fauna is evi-
denced in the most unequivocal manner by a portion of the collection
now described. Cytherea planeta is very closely allied to C. ery-
cma; Cardium hngua-leonis is nearer to C. rubicundum of Madagascar
than it is to C. elongatum of the West Indies ; and so on with several
of the species. But it must not be overlooked that while there is
undoubtedly a closer resemblance of a part of the mollusca to living
eastern forms, than to living West Indian forms, another part of the
fauna presents nearer affinities to that now inhabiting the contiguous
waters. Again, a certain number of the species (¢. g., those of the
genera Cassis, Cassidaria, Conus and Natica) seem to have their
nearest congeners in the European early and middle Tertiaries.

I shall mention another point which has some bearing on the affini-
ties of faunas distant in time and inspace. Mr. Jenkins has shown me
-asmall collection of fossils from Travancore, in the Society’s Museum.
These fossils seemed to me to be probably of older Pliocene or Upper
Miocene date; but without prejudice to the conclusions which may
be arrived at after a closer examination of the fossils in question, I
may state that several of them appeared to me to have near resem-
blances to species now existing in the West Indies. From this it
would appear that while the fauna of the West Indies in Miocene
times appears to have been more closely related to the existing

1866. | GUPPY—JAMAICAN MOLLUSCA. 285

eastern fauna than it is at present, there was a fauna in the eastern
area during some part of the Tertiary Period with a stronger resem-
blance to that of the present Caribean seas than now exists. Thus
these various geologico-geographical groups bear a somewhat similar
sort of affinity to one another, that we find displayed between certain
recent and fossil species of animals. |

When taken as a whole, the resemblace of the Caribean Miocene
fauna to that of Bordeaux, Dax, and Malta is striking, and it is
closer than its likeness to the American Miocene*. The present
molluscan fauna of the West Indies is not altogether devoid of affi-
nities to that of the Mediterranean, and even to that of the Red Sea.
Several of the species are, if not identical, at least so near, that they
are known by the same names. Hence arises some of the confusion
with respect to localities that we occasionally find in conchological
books ; the same species being attributed in one to the Mediterranean
or to the Red Sea, in another to the West Indies.

The series of mollusca now described, with those previously de-
_ seribed by Mr. Sowerby, and the corals published by Dr. Duncan,
will furnish a basis for future investigations into the geology of the
Tertiary formations of the West Indies and Tropical America, and we
may expect conclusions of no small interest therefrom.

§ 2. List oF SpPEcIEs.

Distribution.
; 3 |. &
Species. a [gales
$8 | 28/28) Fossil, Other localities.
me |)aS5|eA
nm
WHRSig SUICHICKA, SOW. ..scccccicecser|acrsceleceees x
MOMUUeLA, GUPPI.c0scceerccilavevar|-orses|eceee-
Malea camura, Guppy .........0..|eeceseleccsceleceee-
Cassidaria sublavigata, Guppy ...jecesse[ecseeefeceees
Strombus pugilis, Lzn2............. 9M llc nahi eleics Cuba ; Anguilla.
BuUrOns, SOW cseccasitsesenas|s seenh eetgee * | Trinidad ?
Conus planiliratus, Sow. .........J..--.efeeeee *
BOMOMIG, ISOs tocesctw sete oscacs|eoswes Banckel ae
stenostoma, Sow. ......c.scesfeceees pat ae
eranozonatus, GUPPY ......|esveeelerceeefeeeees
—— interstinctus, Guppy......c..jeereeefeceees *
gracilissimus, Guppy .....-|.-.+-- Ss Eee
Murex Domingensis, Sow..........J....6. x | *
Persona simillima, Sow............:feceees * *
Ranella crassa, D7llw.............00- Seromlsena saa eck:
Oliva reticularis, Lam. ...........- Reed (ach aatliteas os
Mitra Hlenekeni, Sow. ........00s.feerses|oon oes *
Fasciolaria semistriata, Sow.......|....s-Jeceees x Ke
Latirus infundibulum, Gael. ...| * |...e x | N. America.

* By this I mean that there is such a number of types common to the Mio-
cene of Bordeaux, &c., that they resemble deposits formed within the same great
zoological province. It is in this respect that the resemblance is less close with
the American Miocene.

[Feb. 21,

236 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
List or SpEcIES (continued ).
Distribution.
2)
Species. #floaloe
8 B di 2 E Fossil. Other localities.
ioe] AS BA
mM
Marginella coniformis, Sow. ......|....-. %
Columbella ambigua, Guppy......|......|ss0se0|+0
pradata, Guppy co toe cleeie *
Cancellaria Barretti, Guppy ......|..0.0.|...+--
Igevescens, Guppy Irises. stelreneen| 008
MiGorel, “Guppy. es attacrd telnetes *
Pleurotoma consors, Sow. .........[ececee[ecsees
VOEMUSEUME WSOWs 2.2. ..58 eae es velaeeegloae eee
—— Barretti, Guppy.........0.2.. feces *
— Jamaicense, Guppy .........fececefeeeeee
Terebra inzequalis, Sow.............Jes.0.- %
Phos Moore, Gppy 2 -.e2so.2 eealeeeean| sens
CleBaISs MG UP PU ie dea heer ca |eeine ee eae
Cerithium plebeium, Sow. .........J...s0e|e.seee
Natiea subclausay, Soe a: 2hne spate cb aaelatee ee
SUlCAta ORR eater: seen ae * %
—— mammillaris, Zam. ......... A Sg a
—— phasianelloides, @’ Ord. ......)......)..000- Cuba; Anguilla; Trinidad.
Turbo castaneus, Chemn. ......... * %
Solarium quadriseriatum, Sow. ...|......|...... Anguilla; Trinidad.
Cyclostrema bicarinata, Guppy...|......
Neritina Woodwardi, Guppy ...|......Jeceves
Dentalium dissimile, Guppy ......J...0.-|...05-
Vermetus papulosus, Guppy ......|..-.--|..+.+-
Venus paplia, M7777 ee. ee ane * | * Vienna.
Woodwardi, Guppy .........)...0+- *
Cytherea planivieta, Guppy ......|......|...+ ~
carbasea, (G7ppgy” wa ctscee calor alee ect
Lucina Pennsylvanica, Linn....... ne ss Piedmont ; N. America,
Cardita scabricostata, Guppy ...|......Je00..-
Cardium Haitense, Sow. ....::...|...... %
lingua-leonis, Guppy........ big gaas Mliscatcot
inconspicuum, Guppy ..... ileal Ree
Corbula viminea, Guppy) ....2...i|iiel2sencces
Pectunculus pennaceus, Lam. ...| * |......{.-.00
acuticostatus, Sow. .........|.2.... %
Area consobrinma, S0w: i.e seers *
Noe) [E2700 ce eee oe ee
inzequilateralis, Guppy...... eet
Pecten exasperatus, Sow. ......... Oe fornia Paoc
Tagequalis, WSO, c./ccetemen cal Saaeealee sees
Chama arcinella, Lam. ............ Sea eee N. America.

~§ 3. Description oF THE SPECIES.

1, CASSIS SULCIFERA, Sow.

— Quart. Journ. Geol. Soc. vol. vi. p. 47, pl. 10. f. 1.

‘A form allied to the recent

CO. tuberosa.

1866. | GUPPY—JAMAICAN MOLLUSCA. 287

2, CAssIs MONILIFERA, spec. nov. - PL, kV iens)

- Shell ovate, scarcely ventricose; whorls 5, varices few (1-2) or
none; ornamented with obsoletely nodose, low, round, spiral ridges,
and bearing on the superior angle a somewhat moniliform row of
tubercles ; spire small, conic; columellar callus granose; outer lip
thickened and dentate ; columella very tortuous beneath the callus ;
canal recurved:

Allied to C. LG take Lam. (recent), and still closer to C. diadema,
Defr. of the Bordeaux Miocene.

3. MaLEa cAmuRA, spec. nov. Pl. XVII. fig. 9

Shell ovate, ventricose; whorls 6—7, destitute of varices, zoned
by about 16 low spiral ridges; spire short, conic; aperture rather
narrow, outer lip thickened, dentate; inner lip sinuate, dentate ;
columella tortuous, irregularly folded or plaited; callus thin.

4, CAssIDARIA SUBLHVIGATA, spec. nov. Pl. XVII. fig. 10.

Shell ovate, rimate, striated by transverse grooves which are
decussated by numerous fine longitudinal lines; varices scarcely
prominent, few; whorls 6-7; spire small, acuminate; suture im-
pressed; aperture elongate; outer lip forming a varix which is
scarcely prominent externally, thickened and strongly toothed in-
ternally ; columellar margin covered by a spreading callus, on which
are several folds or plaits; canal short, narrow, slightly reflected.

Allied to the C. levigata, Sow., of the San Domingan Miocene, from
which it is easily distinguished by its short spire and larger size.
Among recent species it is most nearly related to C. striata, but the
shorter spire, among other characters, serves to distinguish it.

a Srrompus PuGILIS, Linn.
Syst. Nat. (ed. 12) p. 1209; Reeve, C. I. Strombus, No. 39.

A common shell in the Caribean Sea.

6. Srromeus BiFrRons, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 48, pl. 9. f. 8.

7. Conus PLANILIRatUs, Sow. Pl. XVI. fig. 7.
Quart. Journ. Geol. Soc. vol. vi. p. 44.

8. Conus soxipus, Sow. PI. I. fig. XVI.
‘Quart. Journ. Geol. Soc. vol. vi. p. 45.

9. Conus stenostoma, Sow. Pl. XVI. fig. 2.
Quart. Journ. Geol. Soc. vol. vi. p. 45.

10. Conus GRANozonatus, spec. nov. Pl. XVI. fig. 5.

Shell elongate, ornamented with numerous (18) transverse nodose
ridges, and longitudinally striated by lines of growth, which are
most distinct in the sulcations between the ridges; uppermost keel
or ridge on the angle of the whorl bearing larger tubercles; spire

elevated, acuminate.

288 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

11. Conus INTERSTINCTUS, spec. nov. Pl. XVI. fig. 3.

Shell obconic, transversely ornamented with many small ridges
bearing moniliform granules, which are most distinct anteriorly,
but become simple striations near the anterior canal; whorls 10,
superiorly carinate; spire rather elevated, acuminate.

12. Conus GRAcILIssimus, spec. nov. Pl. XVI. fig. 4.

Shell elongate, subfusiform, slender, ornamented with flattened
spiral ribs which are crossed by longitudinal striz most distinct in
the interstices of the ribs ; spire elevated, acuminate; whorls angular
above, the angle ornamented with a single row of small obtuse
tubercles; aperture very narrow, elongate; outer lip prominent ;
posterior sinus distinct.

13. Murex DominceEnsis, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 49, pl. 10. fig. 5.

14, Persona simrttma, Sow., sp. Pl. XVII. fig. 13.
Triton simillimus, Sow. Quart. Journ. Geol. Soc. vol. vi. p. 48.

15. Rawewna crassa, Dillw. Pl. XVIII. fig. 9.
Dillwyn, Descr. Cat. 692; Reeve, C. I. Ranella, No. 18.

16. Oxrva RericuLaRis, Lam.
Lamarck, Animaux sans Vert. (ed. Desh.) vol. x. p. 618; Reeve,
C. Ly Oliva, No. wlio,

This species still lives in the Gulf of California, and also in the
West Indies, where it is rather rare.

17. Mirra Henexent, Sow.
M. Henikeri, Sow. Quart. Journ. Geol. Soc. vol. vi. p. 46, pl. 9. £.5.
A small example of this species occurs in the Jamaica collection.

18. FascroLarIa SEMISTRIATA, Sow. Pl. XVI. fig. 12
Quart. Journ. Geol. Soc. vol. vi. p. 49.

19. Latrrvus INFUNDIBULUM, Gmel.
Lamarck, An. s. Vert. (ed. Desh.) vol. ix. p. 386; Reeve, C. I.
Turbinella, No. 3.

20. Marcineria conirormis, Sow. Pl. XVII. fig. 2.
Quart. Journ. Geol. Soc. vol. vi. p. 45.

21. CoLUMBELLA AMBIGUA, Spec. nov. Pl. XVI. fig. 8.

Shell elongate, acuminate, thick, longitudinally ribbed with stout
somewhat undulated coste; whorls about 10, flattened laterally,
eradually increasing ; aperture narrow, outer lip thickened, blunt,
toothed within, scarcely indented by an obsolete posterior sinus;
canal short, recurved; columellar callus with prominent edges.

22, CoLUMBELLA GRADATA, spec. nov. Pl. XVI. fig. 10.
Shell thick, elongate, whorls about 9, flattened and ornamented

1866. ] GUPPY—JAMAICAN MOLLUSCA. 289

above with a series of longitudinally elongate tubercles, and some-
what ribbed near the aperture; the last whorl spirally grooved
anteriorly; spire small, elevated, acuminate; outer lip thickened,
toothed internally; columellar callus with a prominent edge.

This shell is distinguished from the preceding, which it somewhat
resembles, by the middle part of the whorls being smooth, by the
shorter spire, and the somewhat steplike overlapping of the whorls.
Both these species, as well as C. venusta from the San Domingan
Miocene, seem to have relations with Pleurotoma. They belong to
the subgenus Strombina of Morch.

23. CANcELLARIA Barrerri, spec. nov. Pl. XVII. fig. 11.

Shell stout, ovate-turreted, cancellated by numerous equidistant
and close longitudinal and transverse ribs, of which the trans-
verse are somewhat more distinct than the longitudinal; whorls 8,
somewhat compressed, very slightly angulated near the suture ;
aperture ovate, rather narrow: columella strongly folded; outer lip
blunt, very slightly sinuate anteriorly, deeply grooved within.

The specimens seem to be scarcely adult, and the species may,
when full grown, have a columellar callus like that in the next
species.

24, CANCELLARIA LEVESCENS, spec. noy. Pl. XVII. fig. 12.

Shell very thick, ovate, spire cancellated by numerous ribs, of
which the longitudinal are the more distant and more prominent;
whorls 8; last one forming about two-thirds of the height of the
shell, nearly smooth, but with fine lines of growth decussated by low
distant ridges, the latter becoming quite obsolete near the aperture,
except anteriorly, where they are more distinct; aperture widest
anteriorly; columella strongly folded with two very prominent
plaits; callus thick, spreading; outer lip blunt, obsoletely dentate,
grooved internally ; canal short, tortuous.

This species, allied to C. reticulata, Dillw., was at first considered
as a variety of that species, an opinion afterwards abandoned. ‘The
characters given will readily distinguish it from that recent species.
It partakes in some measure of the characters of C. obesa and C. solida,
Sow.

25. CaNncELLARIA Moorst, spec. nov. Pl. XVII. fig. 7

Shell ovate, ventricose, subrimate, longitudinally striated and orna-
mented with stout, rounded, distant, variciform coste, which are
crossed by spiral ribs; whorls about 7, increasing rapidly; aperture
rounded ovate; columellar callus thin, with prominent edges ;
columella twisted, with three plaits; canal neieousse

26. PLEUROTOMA CONSORS, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 50.

27. PrzvRoToma veNnustum, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 50, pl. 10. f. 7

290 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

28. Prevroroma Barrerti, spec. noy. Pl. XVII. fig. 6.

Shell solid, fusiform, elongate, whorls 9-10, carinate, spirally keeled
and striated; keels visible on the upper whorls three, with 3-4
intermediate striz, decussated by lines of growth; second and largest
keel decurrent, with the notch divided by an obsolete groove; aper-
ture elongate; canal long, straight.

A shell like P. wgo, but with more acute keels.

There are some small shells in the collection which I take to be
the young of this species. In these the cross strize between the
keels are more distinct and more delicate.

29. PrevRotoma JAMAICENSE, spec. nov. Pl. XVI. fig. 6.

Shell ovate-turreted ; whorls stoutly transversely ribbed below
the small round keel which follows the suture; the interstices
between the ribs crossed by numerous fine stric, which are decus-
sated by still finer striz ; aperture rather narrow; outer lip some-
what thickened; anterior canal very short; posterior canal scarcely
forming a notch in the peristome.

This shell belongs to a type which has several recent representatives
both in the West Indies and on the West Coast of America. Its
nearest relative is perhaps P. granulosa, Sow., from Panama.

30. TEREBRA INZQUALIS, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 47.

The Jamaican examples are small and fragmentary.

31. Pos Mooret, spec. nov. Pl. XVI. fig. 11.

Shell ovate-turreted, conical, with longitudinal distant ribs which
are cancellated by transverse coste rising into tubercles upon the
longitudinal ribs; whorls 9, rather convex, increasing gradually ;
spire sharp, regularly turreted; aperture ovate; columella some-
what twisted; outer lip internally distantly grooved; peristome
crenate, blunt, somewhat sinuate anteriorly ; canal short, open.

This species is so close to P. Veraguensis, Hinds, that it was at
first considered by Mr. Carrick Moore as a variety of that species ;
an opinion which he subsequently modified.

32. PHos ELEGANS, spec. nov. Pl. XVI. fig. 13.

Shell conical-turreted, elongate, cancellated by longitudinal and
transverse ribs, the latter rising into tubercles upon the former,
which are the largest and most distant; whorls 8, convex, gra-
dually increasing; aperture ovate; columella somewhat twisted ;
outer lip simple, blunt, grooved within.

33. CERITHIUM PLEBEIUM, Sow. Pl. XVI. fig. 9.
Quart. Journ. Geol. Soc. vol. vi. p. 51.

34, Natica susctausa, Sow. Pl. XVIII. fig. 8.
Quart. Journ. Geol. Soc. vol. vi. p. 51.

35. Natica sutcaTa, Bom. PI. XVIII. figs. 14, 15.
NV. cancellata, Gmel.; Reeve, C. I., Natica, No. 95.

1866. | GUPPY—JAMAICAN MOLLUSCA. 291

36. NatIcA MAMMILLARIS, Lam.
Lamarck, An. s. vert. (ed. Desh.) vol. viii. p. 628; Reeve, C. I.
Natica, No. 29. |

I do not feel sure of this identification; but as the fossil seems to
have been referred to this species, I am not at present able to suggest
- an amendment. |

37. NaTICA PHASIANELLOIDES, D’Orb. Pl. XVII. fig. 1.
D’Orbigny, Paléontologie de Cuba, pl. 1. f. 7.

Shell ovate-globose, smooth, scarcely rimate; spire elevated ;
columellar callus narrow, its margin sinuate on the penultimate
whorl.

Although D’Orbigny has not, as far as I can ascertain, pub-
ished any text explanatory of his plates of Cuban fossils, and
although the specimen figured by him is only a cast, I believe the
present shell to be identical with the species to which E have referred
it. It seems to be very characteristic of the West Indian Miocene,
and occurs in a perfect state in San Domingo, and as casts in
Anguilla and Trinidad. The Jamaican example is small, and has
lost its spire. This fossil belongs to that group of Natice so well
represented in the Eocene of Europe by NV. ambulacrum, Sow.,
NV. hybrida, Desh., and NV. acuta, Sow. It has a somewhat taller
spire than any of these. The absence of an umbilicus and the
elevated spire seem to indicate for it a place in the group Amaura,
Moller (1842).

38. TURBO CASTANEUS, Chemn.

The fossil is remarkable for retaining some of the chestnut colour
characteristic of the recent shell with which I am acquainted under
this name. It seems to be the 7’. hippocastaneus of Lamarck. It is
certainly not the form known as 7’. crenulatus, Gmel. (7. articulatus,
Reeve); but whether the latter is to be considered a variety or not,
I am not now prepared to state.

39. SoLARIUM QUADRISERIATUM, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 51, pl. 10. f. 8.

Fine examples of this species occur in Jamaica.

40. CycLostREMA BICARINATA, spec. noy. Pl. XVII. fig. 5.

Shell discoidal, broadly umbilicate; whorls concave beneath, flat
above, with four small spiral keels on the flat upper part, the
periphery formed by two larger and more distant spiral keels,
including between them a somewhat concave smooth spiral area;
peristome continuous.

41. Neririva Woopwarnt, spec. nov. Pl. XVIII. figs. 4, 5.

Shell oval-globose, flattened, with coarse lines of growth; spire
wanting ; mouth very narrow, semilunate ; columella-lip very broad,
flat; columella simple, slightly curved, and furnished with an obso-
lete tooth-like projection anteriorly.

292 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

The spire of the single example has completely disappeared by
erosion, so that nothing but the last whorl is left, and even that
seems to have been somewhat encroached upon by the dissolving
properties of the water in which this mollusk lived. The shell is
different from that of any of the genus I know of inhabiting the West
Indies or South America.

_ 42, DENTALIUM DISSIMILE, spec. noy. Pl. XVII. fig. 4.

Shell subpolygonal and striated at the apex, becoming gradually
round, smooth, and shining near the aperture, which is circular.

43, VERMETUS PAPULOSUS, spec. nov. Pl. XVII. fig. 3.

Shell nearly straight, rather irregularly spirally contorted, orna-
mented with regular longitudinal rows of tubercles interlined with
crenate striz ; aperture subcircular.

44, Venus PAPHIA, Linn.
Syst. Nat. p.1129; Lamarck, An. s.vert. (ed. Desh.) vol. vi.p.371.

45, Venus Woopwarpt, spec. nov. Pl. XVIII. fig. 1.

Shell subtrigonal, somewhat inequilateral, anteriorly rounded,
posteriorly somewhat angulated ; ornamented with numerous fine
radiating costelle, interrupted by equidistant concentric crenulate
ridges, which are continued across the large lunule ; margin beneath
the lunule internally obsoletely toothed. —

A form allied to V. cancellata, Linn., abundant in the Caribean Sea.

46, CyrHErra (CALLISTA) PLANIVIETA, spec. nov. Pl. XVIII. fig. 3.

Shell inequilateral, transverse, oval, compressed; valves polished,
ornamented with numerous flat, slightly irregular, concentric ribs,
which are much closer than their interstices; umbones prominent,
approximated ; lunule scarcely impressed.

This bivalve approaches closely to C. erycina of the Eastern seas.
It is also allied to C. striatella of the Belgian Tertiaries, and even
more closely to C. erycinoides of the Bordeaux beds,

47, CytTHEREA (CIRCE) CARBASEA, Spec. nov. PI. XVIII. fig. 13.

Shell rounded, rather inequilateral, tumid, sulcated by lines of
growth decussating with numerous radiating strive, which divaricate
on the anterior part of the disk, and become subrugose towards the
posterior margin; lunule large, scarcely distinct; posterior margin
rounded; anterior margin somewhat produced.

The character of the ornamentation in this species approaches to
that of C. divaricata, Chemn., and in general form it is related to
that species and to several others of the same group inhabiting both
the eastern and western seas, or found fossil in Tertiary formations.

48. Lucrva Pennsyivantca, Linn.
Syst. Nat., p. 1134.

This well-known species is also found fossil in the Miocene deposits
of Piedmont and of North America. —

1866. ] GUPPY—JAMAICAN MOLLUSCA. 293

49, CARDITA SCABRICOSTATA, spec. noy. Pl. XVIII. fig. 10.

Shell suborbicular, nearly as high as wide, with about 18 regularly
nodosely muricate impressed ribs; posterior margin nearly straight,
forming an angle with the ventral margin, which is rounded; ante-
rior margin rounded ; umbones prominent ; margins strongly crenate ,
hinge with two teeth, of which the posterior one is long and narrow.

50. Carprium Hartensez, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 52, pl. 10. fig. 11.

51. CaRDIUM LINGUA-LEONTIS, spec. nov. Pl. XVIII. fig. 7.

Shell elongate, subquadrate; valves deep, ornamented with nume-
rous (32) nodosely muricate ribs, which are lower and more distant
towards the anterior and posterior margins; margins coarsely cre-
nulate, the posterior one strongly serrate: hinge with three large
and stout teeth. |

The nearest ally of this shell is C. rubicundum of Madagascar. It
is distinguished both from that species and from C. elongatwm by its
deeper valves and by the ribs on the disk being somewhat muricate.
It is also rather narrower than those species.

52. CaRrDIUM INCONSPICUUM, spec. nov. Pl. XVIII. fig. 12.

Shell elongate, subtrigonal, ovate, ornamented with numerous (38)
imbricate radiating ribs broader than their regularly squamose in-
terstices; umbones scarcely prominent; margins strongly dentate ;
hinge small, with three teeth.

53. CorBULA VIMINEA, spec. nov. Pl. XVIII. fig. 11.

Shell thick, transversely oblong, rounded anteriorly, produced
posteriorly into an acute beak; valves ornamented with stout, rather
round, concentric ribs; hinge with a single prominent tooth and a
deep orbicular pit in front of it.

54, PrcruncuLus PENNACEUs, Lam.
: Lamarck, Anim. sans vert. (ed. Desh.) vol. vi. p. 490; Reeve,
C. I. Pectunculus, No. 24.

55, PEcruNncuLvs ACUTICOSTATUS, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 53, pl. 10. f. 18.

56. ARCA CONSOBRINA, Sow.
Quart. Journ. Geol. Soc. vol. vi. p. 52, pl. 10. fig. 12.

57. Arca Noa, Linn.
Syst. Nat. p. 1140; Reeve, C. I. Arca, No. 72.
Abundant in most of the West Indian later Tertiaries, and in the
existing seas.
58, ARCA INEQUILATERALIS, spec. nov. Pl. XVIII. fig. 2.

Shell transverse, slightly oblique, very inequilateral, produced
posteriorly ; valves with about 30 crenate radiating ribs, single on

294 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

the disk, where they are not broader than one-third of their inter-
stices; double anteriorly and posteriorly, where they are equal in
width to the interstices; hinge-line long, straight, forming an
abrupt, angle with the rounded anterior margin; posterior margin
with an oblique slope.

59, PECTEN EXASPERATUS, Sow.
Sow. Thesaurus Conch. vol. i. p. 04, pl. 18: £. 183262 Reeve,
C. I. Pecten, pl. 2. f. 7 & 8.

This Pecten still hves in the West Indian seas. The fossil has
20 ribs, and is slightly longer than the recent shell; but J cannot
regard the differences as specific.

60. Precten Inmevaris, Sow. Pl. XVIII. fig. 6.
Quart. Journ. Geol. Soc. vol. vi. p. 52.

61. CHAMA ARCINELLA, Lam.

The Jamaican shells do not differ from the recent examples; but
the San Domingan specimens may be considered a variety. The
former have more numerous imbricating subtubular spines, which
in the latter are not so regularly arranged in rows, and assume
more the character of coarse squamose granules.

EXPLANATION OF PLATES XVI.-XVIII.
(Illustrative of Tertiary Shells from Jamaica).

Puate XVI.

Fig. 1. Conus solidus, Sow.

2. stenostoma, Sow.
interstinctus, Guppy.
gracilissimus, Guppy.
granozonatus, Guppy.
6. Pleurotoma Jamaicense, Guppy.

7. Conus planiliratus, Sow.

8. Columbella ambiqua, Guppy.
9. Cerithium plebecum, Sow.
10. Columbella gradata, Guppy.
11. Phos Mooret, Guppy.

12. Fasciolaria semistriata, Sow.
13. Phos elegans, Guppy.

3
4,
5

- Prats XVII.

Fig. Natica phasianelloides, d’Orb.
Marginella coniformis, Sow.
Vermetus papulosus, Guppy.

4. Dentaliwm dissimile, Guppy.

5a, 5.b.. Cyclostrema bicarinatum, Guppy.
6. Pleurotoma Barretti, Guppy.

7. Cancellaria Mooret, Guppy.

8. Cassis monilifera, Guppy.

9. Malea camura, Guppy.

10. Cassidaria sublevigata, Guppy.
11. Cancellaria Barretti, Guppy.
12. levescens, Guppy.

13. Persona simillima, Guppy.

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1866. ] GUPPY—WEST INDIAN BRACHIOPODA. 295

Prats XVIII.

Fig. 1. Venus Woodwardi, Guppy.
2. Arca inequilateralis, Guppy.
. Cytherea (Callista) planineta, Guppy.

| Neritina Woodwardi, Guppy.

. Cardium lingua-leonis, Guppy.

. Natica subclausa, Sow,

. Ranella crassa, Reeve.
10. Cardita scabricostata, Guppy.
11. Corbula viminea, Guppy.
12. Cardium inconspicuum, Guppy.
13. Cytherea (Circe) carbasea, Guppy.
14 & 15. Natica sulcata, Desh.

3
4
5.
6. Pecten inequalis, Sow.
7
8
9

2. On Terttary Bracuroropa from Trinipap. By R. J. Lecumere
_Gurry, Esq., Civil Service, Trinidad. ;

(Communicated by the Assistant-Secretary).
[Prats XIX., Figs. 1-3.]

Tuer three species of Brachiopoda which form the subject of the
present communication, were obtained from the gypseous marls con-
taining Orbitoides Mantelli and Nummulina, exposed near the town
of San Fernando in Trinidad*. I have alluded to these beds in my
papers on the Mollusca of Jamaica and on the Echinodermata of the
West Indies. The Gasteropoda and Conchifera contained in these
deposits, are for the most part in bad condition, and generally spe-
cifically indeterminable ; but in the papers alluded to I have given
the names of such species as I have been able to determine. | I have
not found any form which could be referred with any degree of pro-
bability to recent species ; and this circumstance combined with the
stratigraphical position of the beds, the occurrence of Hchinolampas
ovum-serpentis, the great development of Orbitoides Mantelli, &e.
have led me to believe that these strata belong to a lower horizon
in the Miocene series than the deposits in Jamaica, Cumana, and
Cuba. The evidence furnished by the Brachiopoda now described,
ean hardly be considered to throw much new light upon the ques-
tion. ‘They seem, indeed, to be suggestive of Cretaceous affinities ;
their resemblances to known Tertiary and recent forms not being very

pronounced.

It has been suggested to me that, considering the apparent Me-
sozoic type of these Brachiopoda, they may be derivative fossils, but
I see no ground for this supposition. The specimens are not in con-

dition to warrant such a presumption; they do not occur near the

base of the series exposed at San Fernando; they are referable to a
genus still existing, and represented in Tertiary rocks. Besides

which, Mr. Barrett has discovered similar Brachiopoda in the Mio-

* See ‘ Geologist,’ vol. VII., p. 159.

296 PROCEEDINGS OF THE GEOLOGICAL SOCTRTY. [Feb. 21,

cene deposits of Jamaica, as stated in a letter of that naturalist quoted
by Dr. Woodward, an extract from which will be found in a note to
my paper on the Jamaica fossils (p. 281). It is even possible that
one of Mr. Barrett’s fossils may be identical with one of the species
now described. At any rate these fossils are interesting as being,
as I believe they are, the first Brachiopoda described from Miocene
beds in the West Indies.

None of the fossils now under consideration at all resemble
Maltese forms; and herein they differ remarkably from many of the
other organic remains from the Caribean Miocene beds, especially
the Echinodermata and the Corals.

All the species have been ascertained to be punctate.

1. TEREBRATULA TRINITATENSIS, spec. nov. Pl. XIX. figs. la, 16.

Shell smooth, gibbous, irregularly pentagonal, somewhat longer
than wide, marked by wide shallow and obscure sulci of growth,
which become finer and more distinct towards the margins; front-
edge nearly straight; ventral valve convex and rounded towards
the beak, flattened towards the front edge; dorsal valve convex,
with an obscure carination radiating to each angle of the front edge ;
beak large, scarcely incurved over the dorsal valve, truncate by
a rather large subcircular foramen, from which a wide and shallow
sulcus extends forwards.

2, TEREBRATULA CARNEOIDES spec. noy. Pl. XIX. fig. 2.

Shell suboval or suborbicular, smooth, striated by fine lines of
growth ; ventral valve convex with a tendency to carination along
its mesial portion from the beak to the front margin; dorsal valve
rather evenly convex, with an obscure slightly raised mesial fold;
front margin rounded or somewhat produced; beak small, scarcely
curved.over the umbo of the dorsal valve, pierced by a very small
foramen.

The front margin of the example figured is imperfect, but in
another less perfect specimen it is more folded and produced, giving
a suboval shape to the shell. The first-mentioned example resembles
in some respects 7’. carnea from the chalk.

3. TEREBRATULA LECTA, spec. nov. Pl. XIX. fig. 3.

Shell suboval, smooth, suleated by lines of growth which are
strong and well marked towards the margins, and which are crossed
by obsolete radiating grooves; front edge plicate and sinuate ; ven-
tral valve somewhat compressed, especially towards the front margin ;
dorsal valve convex, with a slightly raised mesial foid; beak
scarcely incurved, truncated by a large circular foramen.

Nore on the Forneoine Parrr. By T. Davinson, Esq., P.R.S.5 Ete

Tne subject relating to Tertiary Brachiopoda is one of considerable
importance, since the fossils of this period, taken under the ‘ homo-
taxeous’ view, connect the Cretaceous with the Recent fauna. A

1866. ] GUPPY—WEST INDIAN ECHINODERMS. 297

general monograph of Tertiary Brachiopoda is consequently a great
desideratum.

With regard to the special subject of Mr. Guppy’s paper, the
author is quite correct while observing “ that the evidence furnished
by the Brachiopoda now described can hardly be considered to throw
much new light upon the question, as they seem indeed, to be sug-
gestive of Cretaceous affinities ;” but I might add that their shapes
are not, however, inconsistent with what we might likewise expect
to find in Tertiary formations.

Terebratula Trinitatensis and T. lecta of Guppy are not known to
me as Miocene shells, and may be new; but it must be confessed
that 7’. carneoides, Guppy, strongly recalls to my mind the Cretaceous
T. carnea, as well as the recent 7’. wtrea. Indeed the shell now
termed 7’. carneoides seemed to me identical in shape and foramen
with that of many Cretaceous specimens of 7’. carnea, as well as of
the recent 7’. witrea ; and it may be asked whether 7. vtrea and 7’.
carnea are really distinct species. Their shapes are very often
identical and undistinguishable, their interiors so likewise ; and we
find similar shells, identified as 7’. vitrea by Philippi and Sequenza, —
from the Miocene, Pliocene, and Pleistocene beds of Sicily.

I may here suggest the hope that further researches may be made
in connexion with the beds and fossils in question, as it is always
hazardous to describe so-called new species from the study of a few
specimens, and especially so when the forms are undescribed.

EXPLANATION OF PLATE XIX. figs. 1-3.

(Iltustrative of Tertiary Brachiopoda from Trinidad.)
Figs. 1 a,1 6. Terebratula Trinitatensis, Guppy.
2. —— carpeoides, Guppy.
3. lecta, Guppy.

3. On TertiaRy EcHinopEerms from the West InprEs.
By R. J. Lecumerse Guppy, Esq., Civil Service, Trinidad.

(Communicated by the Assistant-Secretary.)
[Puare XIX. figs. 4-8.]
§ 1. GenERAL Remarks.

Tu Corals of the Miocene formations of the West Indies having
been made known by the researches of Mr. Lonsdale and Dr. Duncan,
the Shells having been in part described by Messrs. Carrick, Moore,
and Sowerby, and a notice of the Foraminifera having been given by
Professor Rupert Jones, I propose to bring under the notice of the
Geological Society the Echinoderms belonging to the same fauna.
The Echinoderms about to be noticed are found in the island of
Anguilla, and in Trinidad, associated with remains which leave little
doubt of their Miocene age. Two of them are identical with Maltese
species, and three more are found living in the West Indian seas.
VOL, XXII.—PART I. Y

298 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

Three others seem to be new, and I have therefore appended de-
scriptions of them.

In Anguilla the fossil Echinoderms occur in a white marly lime-
stone, in which are found numerous remains of mollusca, chiefly as
casts. Several of the mollusca are identical with species found in
San Domingo, Jamaica, and other West Indian Miocene localities.
The most noteworthy are Natica phasianelloides, d’Orb., Solarium
quadriseriatum, Sow., and species of Turritella and Pecten. Teeth of
Pyenodont fishes also occur in the beds, as in Malta, and among them
is one apparently very closely allied to Spherodus gigas. Several of
the other mollusca are probably identical with those of the West
Indian localities mentioned; but it would be hazardous to speak
precisely, where the only materials are imperfect casts.

In Trinidad the fossil Echinoderms are found in highly inclined
gypseous marls, often impregnated with asphalte, and with occasional
partial dark-blue limestones exposed in a cliff section at San Fernando.
The mollusca are numerous, but most frequently in a very imperfect
condition ; the metamorphism induced by the change of the gypsum
into selenite, having frequently obliterated and destroyed their shape
and characters. Of those that are recognizable we have the Natica
phasianelloides, d’Orb., found in San Domingo, Jamaica, Cuba, and
Anguilla, and an unnamed Jurritella, found in Jamaica, San Do-
mingo, and Cumana. Among the Foraminifera we have Vummulina,
Orbitoides Mantelli, and Heterostegina. The two former occur in
great numbers*, and the Orbitordes are well developed. EHchino-
lampas ovum-serpentis is the most common Hchinoderm here, and it
seems to have been a remarkably variable species. The only other
Echinoderms found at San Fernando, are a small species of Echinus(?),
and some stems of Crinoids, all too imperfect for determination.
Two or three species of Terebratula are also associated with these
fossils.

At Anguilla remains of a large star-fish are found, which may
have belonged to an Astropecten.

In addition to the Echinoderms now made known, several have
been previously published, some of which may be from Miocene
strata. D’Orbigny has described a fossil, from beds in Cuba which
I take to be Miocene, under the name of Periastes Cubensrs, while
Michelin and Duchassaigne have published some species from
Jamaica and Guadeloupe. I am not, however, acquainted with those
species. ;

7 Out of the nine echinoderms which I have determined, three only
are new, while two occur in the Maltese beds and in other Miocene
localities in Europe. Three more which occur rarely in the fossil
state are still existing in West-Indian seas. Though the test of
numerical proportion can scarcely be applied to so small a number
of species, there is enough evidence to justify us, taking the associated
mollusca and foraminifera into consideration, in concluding that the
formations in Anguilla and Trinidad, whence these fossils are derived,

* Geologist, vol. vil. p. 159.

1866.] GUPPY —WEST INDIAN ECHINODERMS. 299

are of Miocene age. And it is not surprising, after the researches of
Dr. Duncan and Professor Rupert Jones, to find so remarkable an
alliance with the Maltese beds. From the evidence furnished by
the organic remains, I have-been led to consider the Anguilla and
San Fernando beds as probably somewhat older than the middle
Tertiaries of Jamaica, Cumana, and San Domingo, and I have men-
tioned this part of the subject in my paper “ On the Tertiary Mollusca
of Jamaica.” Only two or three species appear, as far as my re-
searches have gone, to pass through the entire Miocene ; nevertheless
the whole fauna is so closely connected throughout by intermediate
links, that the separation of the West Indian Miocene into upper and
lower, can only be effected in a general way.

§ 2. DESCRIPTION OF THE SPECIES.

1. Crparts merrrunsts (Forbes), Wright.

i ea Ann. & Mag. Nat. Hist. 2nd ser. vol. xv. p. 107, pl. 4.
fig.
Eeeatiy. Anguilla.

2. EcHINOMETRA ACUFERA, Blainville.

The fossils only differ from the recent examples in that the former
are smaller; but they agree perfectly with living examples of the
same size.

Anguilla.

3. CLYPEASTER ELLIPTICUS, Michelin.

Michelin, Monogr. des Clypeastres fossiles (Mém. Soc. Géol. de
France, 2nd ser. tome 7), p. 109, pl. 12.

«« This species, near to C. rosaceus, differs from it in that it is less
elevated, has no marginal sinuosities, and that its ambulacra are
rather elongate than rounded towards the base” (Michelin, J. c.).
It appears to me to be more nearly related to C. australasia, Gray,
than to C. rosaceus, and I have had some doubt whether it ought
to be accounted distinct or not. It agrees with C. australasia, in
having the base concave from the margins, and in others respects in
which these species differ from C. rosaceus.

This is a common species at Anguilla. I am not aware of the age
of the deposit from which Michelin obtained his fossil.

4, EcHINOLAMPAS SEMIORBIS, spec. nov. Pl. XIX. fig. 7

Test large, discoidal, nearly circular, very slightly wider behind
than before, subconical; ambulacral summit nearly central; ambulacra
not petaloid, extending nearly to the margins; single ambulacrum
scarcely narrower than the others; poriferous avenues about one-
fourth the width of the interporiferous areas; base somewhat concave,
slightly swollen in the interambulacral spaces ; oral aperture large,
transverse, nearly central, with deep notches opposite the terminations
of the rows of pores. Anus large, transverse, close beneath the
margin.

y¥2

300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 21,

Secondary granules none or indistinct ; primary tubercles simple,
deeply sunk, and very numerous and close-set towards the margins,
becoming more dispersed towards the peristome. The ambulacra
are somewhat raised above the general upper surface of the test;
the pairs of pores are connected by oblique grooves; the inner pores
are round, the outer ones slit. The general form is nearly hemi-
spherical, the antero-posterior but slightly exceeding the transverse
diameter, and the test being only slightly wider behind. The height
is about equal to half the transverse diameter.

This species is closely allied to #. hemisphericus, Lam., and it
differs from that species chiefly in having more numerous and closer
primary tubercles, in the more open and less petaloid ambulacra,
and in having a large transverse vent. H. hemisphericus is found in
the miocene of Malta, and other localities. £. semiorbis occurs at
Anguilla, and it is used as a pound weight by the inhabitants.

5. EcHINOLAMPAS LYCOPERSICUS, Spec. nov. Pl. XIX. fig. 8.

Test oval, wider behind than before; upper surface convex,
margins tumid; ambulacral summit subcentral; ambulacra raised,
petaloid, extending nearly to the margins, base concave towards the
subpentagonal mouth; tubercles small, numerous, and very closely
set, becoming large and somewhat more scattered towards the mouth,
which is subexcentrical and slightly notched by the termination of
the rows of pores continued from the ends of the ambulacral petals ;
anus large, transverse, oval, closely submarginal.

The nearest species to this is Z. scutiformis, Leske, found in Malta
and elsewhere. The present species is constantly smaller, and the
ambulacra appear to be longer and the summit more median. The
dorsum is more equally inflated, and there is no tendency to a sub-
conical form.

Anguilla.

6, ECHINOLAMPAS OVUM-SERPENTIS, spec. nov. Pl. XIX. figs. 4-6,

Test oval, subcylindrical or nearly circular, wider behind than
before, slightly rostrated anteriorly and truncate posteriorly, some-
times having a tendency to become polygonal; ambulacra raised,
petaloid, open at the ends, extending nearly to the tumid margins,
the pores connected by an oblique groove; base convex, except
towards the mouth, where it becomes somewhat concave ; dorsum
rather evenly convex; ambulacral summit subcentral; anus small,
circular, situate between the peristome and the nae much nearer
to the latter than to the former.

This seems to be an extremely variable species, both as to seithed
shape and as to the form of the mouth. It is distinguished from the
preceding by its small circular vent and wider ambulacra. The
mouth is usually subpentagonal, but occasionally becomes transversely
oval. Some examples which approach the circular form have a
tendency to become subconieal.

San Fernando, Trinidad.

1866.] YOUNG—PLATYSOMUS. 301

7. Ecuinonevs cyciostomvus, Leske.

The very wide geographical distribution of this echinoderm prepares
us to expect to find it in a fossil state. It seems, however, to have
been rare in the Miocene period, compared with Echinolampas lyco-
persicus and Schizaster Scille.

Anguilla. The single example I obtained is very small.

8. Scurzaster Scirua, Desmoulins.
Anguilla. Rather common. It is also found in the Maltese beds,

9. Brissus pruritus, Agassiz.

Found in Anguilla. The fossil is, if I have correctly determined
it, identical with the species living in the adjoining seas. It is very
rare as a fossil at Anguilla.

EXPLANATION OF PLATE XIX. figs, 4-8.
(lllustrative of West-Indian Tertiary Echinoderms.)

Figs. 4a, 4b. Echinolampas ovum-serpentis, Guppy. Natural size.
5. A small example, showing the position of the vent
and pentagonal mouth. Natural size.

6. ————. Acircular form with ovate transverse mouth. WNa-
tural size.

(f seniorbis, Guppy. One-half the natural size.

8. lycopersicus, Guppy. Natural size.

4. On the Arrinities of Puatysomus and ALLIED GENERA. By Joun
Youne, M.D., F.G.S., of the Geological Survey of Great Britain.

(Communicated by Professor Huxley.)
[Puates XX. & XXT.]

Tur genus Platysomus, as defined by Agassiz, and placed by him
among the heterocercal Lepidoids with flat broad bodies, contains
forms which cannot be included under the definition he has given.
The imperfect materials from which his descriptions were drawn
up have since been supplemented by abundant well-preserved speci-
mens, whence it is comparatively easy to fill up the masterly outline
he has sketched in the ‘ Poissons Fossiles.’

The first change in the classification of the group to which Platy-
somus belongs was proposed by Sir P. G. Egerton (Quart. Journ.
Geol. Soc. v.). The occurrence in a mandible of Pl. macrurus, Ag.,
of teeth with a blunt conical crown and constricted neck, and the
discovery of the true nature of the apophyses (compared by Agassiz
to the V-shaped bones of Clupea), suggested the affinity of that
species to the Pyenodonts, to which family, therefore, Sir Philip re-
ferred the whole genus, and along with it Globulodus, Minst.,
whose relation to Platysomus, Agassiz had previously suspected.
This change Agassiz accepted. But the ‘‘ dents en brosse ’’ mentioned

302 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 21,

in the generic definition (Poiss. Foss. ii. p. 6) and in the description
of Pl. gubbosus (ibid. ii. p. 165) are not Pycnodont but Lepidoid
(=Lepidosteid). The former family was thus made to include two
distinct types of dentition, associated, as will appear, with equally
distinct osteological characters. Thiolliére in a remarkable paper
“On the Jurassic Fossil Fish of Bougey” (Bull. Soe. Géol. France, 1858,
xv. p. 372) alludes to the vagueness of the definition of the Pyc-
nodont family, whence, he thinks, should be excluded Platysomus,
Tetragonolepis, Phyllodus, &c., whose reference to that natural group
is based, he says, ‘‘on insufficient or deceptive analogies.” Cocchi
has since (Nuova Famiglia di Pesci Labroidei, 1865) given good
reasons for removing Phyllodus to the Labroide:. The place of Te-
tragonoleprs is undoubtedly among the Lepidosteide.

Professor Huxley having kindly given me access to the specimens
under his care, specimens obtained for the most part by Mr. Moly-
neux of Burton-on-Trent, I have had very favourable opportunities
for studying the genus Platysomus. I am also indebted to Mr.
Ward of Longton, and Mr. Garner of Stoke-on-Trent for the libe-
rality with which they lent for examination many nearly perfect
specimens from their cabinets, and to Mr. Davis for his assistance
when examining those in the National collection.

The Pyenodont family is characterized by teeth adapted for
crushing, which consist of a circular or transversely oval crown,
flattened above, and sessile on the bone to which it is attached; or
of an obtusely conical crown which is broader than its peduncle of
support.

The teeth in the Carboniferous genera which form the subject of
this paper present three types; Ist, the sharply conical tapering
teeth common to most Lepidosteids; 2nd, the blunted cones with
constricted necks; and 3rd, a series of dental tubercles of peculiar
ultimate structure.

To the species presenting the former type of dentition, I propose
to restrict the generic name Platysomus. The genera presenting
the second type are, equally with the former, but in a different di-
rection, transitional to the Lepidosteede; while the genus Amphi-
centrum, mihi, in which the dental tubercles occur, is distinct from
the Lepidosteids on the one hand, and, on the other, from the Pye-
nodonts properly so called.

Puatysomus, Agassiz, partum.

Body flat, broad. Head triangular, higher than long; snout
sharply angular. Premaxilla small; maxilla in a single piece;
mandible slender, spatulate ; all three bones armed with fine, conical,
sharp teeth. Branchiostegal rays few, enamelled. Interopercular
wanting. No ventral fins. Dorsal and anal fins opposite; their
bases extended, and nearly equalin length. Tail heterocercal, equi-
lobate. Scales oblong, vertically striated, with moderately strong
lepidopleura. The marginal scales anterior to the opposite fins,
more or less modified. Notochord persistent; arches ossified.

The genus thus defined includes Pl. gubbosus, rhombus, striatus (?),

1866. ] YOUNG — PLATYSOMUS. 303

and parvulus. Pl. parvus has been merged by King (Permian
Fossils) in Pl. striatus ; Pl. intermedius, Minst., by Geinitz in Pl.
gibbosus ; and Pil. Fuldar, Minst., by the same author, in Pl. macrurus.

Piatysomus PARVULUS, Ag.

Body with a gentle ventral convexity ; the dorsal highest point an-
gular, anterior to the middle of the back. The nuchal margin nearly
in a line with the slope of the face. Head triangular ; its length equal
to one-fourth of that of the body. Orbits of moderate size and close
to the upper margin of the head. Jaws armed with slender conical
teeth, those in the lower slightly larger and more distant than those
in the upper jaw. Facial and opercular bones vertically striated ;
cranial bones and mandibles finely tuberculated. Pectoral arch
moderately strong; fin with narrow base, and expanded rounded
extremity. The dorsal commences at or behind the middle of the
back, slightly in front of the anal, and terminates opposite the latter
at the caudal root ; the anterior rays are, in both, the longest, the
others abruptly shorten and maintain nearly the same length back-
wards; the former bifurcate only at their extremities, the latter
divide repeatedly, forming a fine fringe. Tail heterocercal, equilo-
bate. The anterior margins of all the fins are protected by fine
fulcral scales ; the nearly square articles of the rays are covered by
striated scales. ‘The scales are oblong, higher than broad, they
diminish in size towards either margin of the body and towards the
tail. They are ornamented by parallel vertical strie, which are
rather more than their own breadth apart, and have their crests
finely tuberculated. The lepidopleura continue distinct as far as
the root of the tail, whose upper lobe is covered by a single series of
large pointed ridge-scales. The upper and lower edges of the body,
anterior to the opposite fins, are also protected each by a single row
of small scales, modified into smooth tubercles, which support small,
usually recurved, denticles: of these there are generally four on each
ventral, and three on each dorsal tubercle. With these tubercles
the lepidopleura are connected above and below. The lateral line
is nearest the dorsum, towards which it is gently arched in front,
terminating at the upper angle of the operculum.

PLatTysomus PARVULUS, Var.

The body is more oval than in the typical form above described,
its greatest depth is marked by no angular dorsal peak. The caudal
pedicle is longer. ‘The striz on the scales are finer, barely their
own width apart, and their crests are smooth.

The species was founded by Agassiz on specimens at Leeds, but
was not described by itsauthor. My reference to it of the numerous
specimens from the North Staffordshire Coal-field is confirmed by
Prof. W. C. Williamson, who, in his valuable memoir “On the
structure of Scales and Teeth,’ communicated to the Royal Society
‘in 1849, describes the scales of Pl. parvulus as “ covered with deep
grooves and intervening ridges running nearly parallel with the long
axis of the scale which, as in Gyrodus, really represents its breadth;

804 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

[ =height ?], and is at right angles to the direction of the lateral
line of the fish.”

Figs. 1-4,— Diagrammatic restorations of the heads of (1.) Amphicen-
trum, (2.) Platysomus, (3.) Aichmodus, and (4.) Pycnodus
(after Thiolliére).

Fig. 1. Fig. 3.

,
7 er v
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eet-q------- De K 3 ?
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/ ’ a
,
ye / 5 fi
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~S ‘ J
‘ a =
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¢ Fy |
Mn. * ;
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.

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_ Eth.

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-

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Temp. ----
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Figure 2 is a diagrammatic restoration of the structure of the
head of Platysomus. The occipital crest rises from a narrow bone
(S.0.), lodged between the square parietals (Pa.), and connected in
front with the frontals (f’r.), which, broader behind, narrows in
front, receiving in its outer excavated margin two bones, which com-
plete the orbital circle superiorly. The posterior of these (P.Fr.)
extends to the parietals and thus represents a united postfrontal
and squamosal (mastoid, Cuv.). The anterior frontal (A. Fr.) dips
down, and gives insertion to the narrow suborbital chain which is
attached behind to the P. /r. The anterior frontals of opposite sides

1866. } YOUNG-—PLATYSOMUS. 305

are separated for great part of their length by the frontals, the remain-
ing space being occupied by the ethmoid, a small bone ( 4th.) which
separates the upper ends of the nasals (Na.), two narrow elongate
bones, in contact for great part of their length, and received into
notches of the ascending premaxillary processes. The upper end of
each nasal is dilated into a process separated by a notch from the A.
Fr., and forming the inner wall of the nasal aperture, whose outer
boundary was either a suborbital bone, or was formed by the vertical
portion of the maxilla. The narrow premaxillaries (Pmw.) give off
ascending plates of considerable relative breadth and height, receiving
superiorly the lower end of the nasal bones. The maxillary over-
laps the upper mandibular margin behind, and rises above to a
right-angled triangle, whose apex is at the premaxilla. The spatu-
late mandible (Mn.) is shorter and stouter than that of Paleoniscus,
which it much resembles. The teeth are perfectly smooth. The
suspensorium forms a solid bar, never shares in the dislocations
which have made clear the other head-bones. It consists seemingly
of a hyomandibular (Hy.), preopercular (Pr.O.), and quadrate (Qu.).
If a symplectic were distinct, its structure would coincide with that
of living Teleostex. Ata point corresponding to the upper edge of
the quadrate, traces of the hyoid articulation are frequently seen.
Along the anterior margin of this bar two triangular plates are
applied, the lower is evidently the slightly expanded quadrate; the
upper, part of the palato-pterygoid arch. It is overlapped and
apparently in close union with the maxillary vertical plate, by which
the other members of the arch are concealed, but above whose mar-
gin a long irregular plate appears, which, coming as it does into
relation with the anterior frontal, is doubtless the edentulous palate-
bone (Pl.). The operculum (Op.), shorter but as broad as the
suboperculum (S.Op.), is attached to the hyomandibular, and the
latter to the posterior frontal, thus proving the squamosal nature of
that bone. No remains are preserved of the inferior cranial bones,
which were probably cartilaginous. A bar of bone answers in posi-
tion to the basisphenoid, but is very imperfect, and wants any
sphenoidal expansions. ‘The vomeris rarely seen, but, in a specimen
of Pl. gibbosus (Brit. Mus. 28279.), is provided with a fine brush of
teeth. As many as four similar tufts occur in the Staffordshire
specimens, so as to suggest their pharyngeal position, but the bran-
chial arches are invariably wanting. The numerous occipital plates
of Lepidosteus are not represented unless by some large scale-like
plates, which are probably nuchal, not cranial. The small suprasca-
pular (S.Sc.) is distinct.

The rest of the body presents no points in addition to those already
noted by Agassiz, save that there is no evidence for the existence of
aventralfin. Indeed, perfect specimens demonstrate its absence, and
thus furnish a valuable diagnosis from the Pycnodonts which have it.

The range of the genus is from the Coal-measures to the top of the
Permian. Pl. striatus is the only species common to both periods
and to England and Germany, a specimen from Derbyshire being in
the Jermyn Street Collection.

306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

AMPHICENTRUM, noy. gen. Pl. XX.

Body flat, broad, prolonged into peaks, a dorsal and ventral pro-
tected by indurated scales: the depth of the trunk thus exceeds its
length. The prolongation into the upper caudal lobe is short, and
tapers rapidly. Head triangular, nearly equilateral. Premaxilla
very large, edentulous. Maxille and mandibles very strong: the
opposed: surface of each presents two ridges, on which are inserted
dental plates raised into distant tubercles ; their substance is tra-
versed by large medullary canals, which reach the surface of the
tooth, terminating there in fine pores. The palato-vomerine area is
occupied by a pair of plates bearing, each, three longitudinal rows of
alternating dental tubercles like those of the jaws. Branchiostegal
rays few, enamelled, not projecting below mandible, covered by an
interopercular. No ventral fin: dorsal opposite, and longer than
anal. Tail heterocercal, equilobate. Scales oblong, ornamented, like
head-bones, with tubercles. Lepidopleura very strong, terminating
inferiorly in modified marginal tubercles; notochord persistent, arches
well ossified.

A. eranutosum, Huxley.

This genus is founded on a large number of specimens, all from
the North Staffordshire Coalfield.

The general arrangement of the head-bones (fig. 1) resembles that
of Platysomus, the distinctions in detail are. however, well marked.
The occipital crest is bounded by two parietals. The frontal is very
broad: the anterior and posterior frontals are massive, and project
_ wellover the orbit. Behind the latter, separating it from the pari-
etal, is a strong plate (Sq.), the true squamosal, giving attachment
to the suspensorium. ‘The posterior frontal thus receives only the
hinder end of the suborbital arch. The frontal and anterior frontal,
are both received on the broad end of the hour-glass bone (Zth.)
which abuts against the premaxille, a pair of massive elongated
edentulous bones forming a strong beak: its outer surface is tuber-
culate above, but near the tip covered with compact and smooth
ganoin. The nasals are thrust out laterally, and applied against the
ethmoid, the nasal apertures being completed externally by a plate
from the suborbital ring, which is analogous to a lachrymal in man
Teleosteans. The vertical upper portion of the maxillary (Pl. XX.
fig. 2) bulges below into an abruptly projecting labial mass, whose
oral margin forms a ridge separated by a shallow groove from an
inner ridge. Seen from below, this groove terminates sharply behind
by the approximation of the outer and inner ridges: but is closed in
front by the premaxilla. On the outer ridge the dental tubercles
are few: on the inner, which is more prominent, they are more
numerous, less so however than on the mandible (Pl. XX. fig. 4.),
which is the converse of the maxilla, in that the ridges approximate
in front (the tubercles ceasing before their coalescence), while the
groove is open posteriorly: the outer ridge is also the more prominent,
_ To the naked eye, and even under the lens, no line can be detected
between the substance of the tubercles and that of the jaw. Under

1866. YOUNG—PLATYSOMUS. 307

the microscope*, however, transverse slices of the jaws show that
the two ridges are made up of dentine, and are connected by a thin
layer of the same substance which floors the intervening groove.
The whole plate thus constituted is lodged in an alveolus, whose thin
margins overlap the base of the dental plate, covering the pseudo-
enamel or cement layer which invests that portion of the plate.
The dentine is very finely granular, and traversed by medullary
canals, which are most divergent in the centre of the tubercles. These
canals bifurcate once, seldom twice, and never anastomose. The
branches reach the surface of the dentine, and there terminate in
funnel-shaped pits, similar to those by which they open into the
pulp-cavity. Hach canal is surrounded by an areola of darker colour
than the intervening clear dentinal space. This areola is narrow in-
feriorly, but its area soon exceeds that of the canal, and maintains
this proportion to the surface. The areola is made of tubes which
come off at right angles to the canals, form a fine network, and, at
the margin of the areola, give off finer tubes, which traverse the den-
tine in an obliquely upward direction, anastomosing, without inter-
vening dilatations, with the similar tubes from adjacent canals, so
as to form a network, whose interspaces are diamond-shaped. In
consequence of this upward direction of these fine tubes, a triangular
space is left between the bases of the canals, which is traversed by
vertical tubes springing directly from the pulp-cavity. The canals of
the dentine which floors the median groove are only half the diameter
of those in the tubercles: they are close-set, and connected either
directly, or by the intervention of branches which pass for the
most part at a low angle from the canals. The areola is narrow:
the tubules of the clear space are larger than in the tubercles, and
form a less angular network. These differences in the proportions
of the parts, differences rather of degree than kind of structure,
commence abruptly on either side of a vertical line which may be
drawn from the point where the tubercle begins to rise above the
plane of the groove. At the outer inferior angle of the base of the
dental plate, but not encroaching on the surface which is turned
towards the substance of the jaw, a layer of bony tissue commences
as a thin investment, which rapidly thickens upwards, and appears
above the alveolar margin, it also occupies a part of the surface of
the median groove. Its further extension towards the apex of the
tubercles, or its replacement by a thin enamel layer, of which only
fragments survive, cannot be ascertained; the extreme brittleness
of the specimens prepared for the microscope having rendered the
process of grinding unusually difficult. The pseudo-enamel, or
cement, is divisible into three lamelle, a clearer separating two dark
layers ; all these are more granular than the dentine. The under
surface is projected into conical processes, which fit into the terminal
infundibula of the medullary canals. The tubes given off from these
canals enter the deepest layer of the cement in which they form a
network of equal-sized tubes: this network invades part of the clear

* The details of this interesting dentitional type are reserved for fuller de-
scription and illustration.

308 PROCEEDINGS OF THE GEOLOGICAL SOIETY. [ Feb. 21,

layer, in whose upper portion it breaks up into a series of fine taper-
ing, anastomotic tubules, which seem to open on the outer surface.
The bone on which this dental plate rests presents the usual lami-
nated structure in its deeper portions. Towards its alveolar surface
the lacunee enlarge, and become more spherical: medullary canals
make their appearance, and increase both in number and size up-
wards, the bone occupying a progressively smaller area as compared
with that of the canals. Into each of these canals seldom more than
one of those of the dental plate open, the intervening dentine resting
on, but not being continuous with, the osseous septa. The same modi- —
fication of structure as may be traced from above downwards in the
jaw, is found to occur towards either alveolar margin: the medullary
canals disappear, the lacunze become fusiform, and at length merely
separate lamine of compact bone, which slightly overlaps the lower
lateral angle of the base of the plate.

The osseous matrix is thin in proportion to the height of the tooth.
The surface vertically opposite the intertubercular groove is very
irregular, while the imperfect section of the maxillary vertical plate
shows that it did not increase in thickness inferiorly. The maxilla
was therefore L-shaped. It is evident that a dental plate so con-
structed is unequal to the crushing indicated by the tubercular teeth.
The palato-vomerine plates are also weak for the work for which
they are adapted. It can scarcely be held that the thinness of the
jaws is due to the loss of an articular plate in the mandible, or of
any part of the maxilla. It seems more probable that, as the incom-
pleteness of the basicranial structures points to their cartilaginous
condition during life, so the three tooth-bearing bones are incomplete
by the loss of the cartilaginous cushions on which they rested. That
the premaxilla also received some similar support, is probable from
its fracture showing a thick outer case of bone, inclosing an interior
hollow. | :

This whole masticatory apparatus is very complex in its morpho-
logical relation. ‘The jaw-plates bear some resemblance to those of
Chimeroid fishes, especially Hdaphodon, in which the tooth is
socketed in a jaw of. ordinary osseous tissue; but the medullary
canals of that genus are much larger, and become closed superiorly
by calcification. In Cestracion the calcigerous tubes come off as in
Amphicentrum, but are lost in the superficial dense layer. From
Pycnodonts, the socketing of the teeth of Amphicentrum, the thin-
ness of the enamel layer, the presence of a cement layer, and of
medullary canals are sufficient distinctions. To Psammodus and
Ptychodus the resemblance of the dental plates is closer. In both
these genera, however, the canals are smaller, more numerous,
branch more freely, and terminate by breaking up into tufts of cal-
cigerous tubes, whereas in Amphicentrum no such breaking up
occurs. In the latter, again, the ossified dentine is separated from
the osseous matrix; in the former the two structures are continuous.
The pharyngeal teeth of Sargus and the teeth of Sargodon also offer,
in their mode of attachment and in their minute structure, resem-
blances to the genus under description, which are further made in-

1866. | | YOUNG—PLATYSOMUS, 309

teresting by the jaw-teeth of the living genera having some common
characters with those of Pycnodus. The pharyngeal denticles are
implanted in a matrix of widely cancellated bone, which becomes
dense and lunular towards its alveolar borders. The ossified dentine
is distinct from the matrix, and is not divided into enamel and den-
tine, the outer layer being simply a portion of the tooth-substance,
in which the calcigerous tubes form a fine reticulation. If several
of these denticies were continuous in place of contiguous, the dental
plates of Amphicentrum would be reproduced.

Lying in the wide gape of the large specimen figured are two nar-
row plates, the one in cast only, the other the plate itself (Pl. XX.
fig. 7). On the latter are three longitudinal rows of alternate
teeth, those of the lateral rows not opposite each other, but alter-
nate, hence giving the transverse series a spiral aspect. The plate
is not entire, its limits, therefore, are indeterminable. It is slightly
curved anteriorly, the straight posterior part containing the larger
teeth. These are longitudinally oval, evenly curved in both axes,
the smaller teeth are spherical. Their surface is studded with fine
granular pits, as in Psammodus. Under a lens the tubercles are
structurally identical, and seemingly continuous with the interven-
ing plate, than which they have a more vitreous aspect, as if a
denser enamelloid layer invested their surface. They are, in fact,
to outward appearance the counterparts of the maxillary and man-
dibular apparatus: it is to be regretted that of this structure no
microscopic section can be obtained. The plate, whence the tubercles
spring, is very thin, 4th of an inch in thickness; the under surface
is set with fine, distant, conical pits, to judge by the cast exposed
on the shale. The resemblance to the jaws is therefore considerable,
in the thinness of the osseous layer and irregularity of its under
surface. The anatomical value of this plate is not quite clear. As
no bone corresponding to the edentulous plate in Platysomus is found,
_ these two curved dental plates may, with great probability, be taken
to represent the palato-vomtrine mass. As there seems no reason
for considering the curvature accidental, they differ from the same
parts in Pycnodus, in that their inner margins were not in contact ;
the arch of the palate was, therefore, incomplete, or closed by mem-
branes only; at least there is at present no evidence of a central
series of crushing teeth, or of an unarmed bony plate closing the
gap. A specimen in Mr. Ward’s possession shows that the transverse
breadth of the head is in agreement with the supposition that the
two rami were apart.

The suspensorium is very strong, descending nearly vertically from
the squamosal. The close union of the bones forbids any attempt to say
what were the components of the bar. A pterygoid plate is attached
to it anteriorly and superiorly; but the other constituents of the
palato-pterygoid arch are concealed beneath the maxillary vertical
plate. There is an indication on one specimen, of facial plates over-
lying this vertical portion, as in Tetragonolepis and its allies, parts
in fact of the so-called outer orbital ring; but, if the surmise is
correct, they are in less close relation to the true suborbital ring,

310 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 21,

and contrast very strongly in shape and size with it. The suboper-
cular is the largest of the three bones; the opercular and interoper-
cular are nearly equal ; the latter overlaps the branchiostegals, which
are nevertheless enamelled externally. The suprascapular is well
developed ; the pectoral arch very strong, the so-called coracoid ex-
panding into a wide oval process. The pectoral fins are higher than
usual above the ventral margin; but, relatively to the opercular
bones, they hold the same place as in the majority of the rhombic
fish, namely, opposite the inferior margin of the subopercular.

The peaks into which both margins of the body are produced are
not opposite: the dorsal being slightly in advance of the ventral.
They are formed by a set of gradually narrowing scales, seemingly
denser than the rest, and ending in tolerably sharp recurved points.

From these the posterior slopes are rapid, with feebly convex out-
lines, the anterior more gradual, straight. The scales are very high
in proportion to their breadth on the flanks, and diminish both to-
wards the margins and the tail ; never, however, becoming equilateral,
save on the upper caudal lobe. The series are nearly vertical, thus
leaving, anteriorly to that row skirting the opercular bones, a tri-
angular space, whose upper boundary is the mandible. In this area
the scales are smaller, but longer than broad, and radiate from the
upper posterior corner of the space to the margin of the body. The
ornament consists of a thick ganoin layer, raised into partly confluent
tubercles, after the fashion of Pl. XX. fig.5. In only one specimen
is the evidence distinct of a medification of the marginal scales; in
it those of the ventral edge anterior to the peak have their lower
ends denticulate, but as those denticles are attached to high scales,
there is no single row, those of opposite surfaces alike contributing
to the outline of the trunk. The lepidopleura are very strong, and
are of the structure already so well described by Sir P. Egerton (loc.
cit.). The fins are made up of rays, slender for the bulk of the
animal; the articles are short, and covered with ornamented scales.
They bifurcate successively near their €xtremities into a fine fringe.
The anterior rays of the dorsal and anal are longer than the rest, as
in Platysomus. The anterior rays in all the fins (except the pecto-
rals, whose defective state leaves this point undecided) are fringed
with a fine series of fulcral scales. Those on the upper caudal lobe
are a single row of strong, triangular, peaked scales, with a notched
posterior margin. The lateral line is straight, and passes obliquely
upwards from the tail to the lower opercular margin.

Of the internal skeleton little can be said, save that the processes
are well ossified, and their vertebral ends expanded so as to approach
the half vertebra of the Pycnodonts. The pelvic bones figured by
Agassiz have not been preserved in any specimens I have seen ; and
as they are placed by him in front of the anal fin, it seems likely
that they are in reality suggested by the frequent distortions of the
dorso-ventral scale-rows in that region.

Fragments of this genus are frequent in the North Staffordshire
coal-fields: they also occur, though more sparingly, in the Scottish
coal-fields, especially in that of Lanarkshire.

1866. | YOUNG—PLATYSOMUS. 311

Evrysomus=Puarysomus. Ag. partim.

This name is proposed provisionally for Pl. macrurus, since the
character of its dentition removes it from Platysomus and Amphi-
centrum, with which it shares the common want of a ventral fin.
The scale-character allies it somewhat to the latter genus. Not
having seen, however, the characteristic dentition, I refrain from
offering any generic definition*.

The relations of these three to each other and to other genera are
somewhat complicated. The structure of the head is, in all three,
strikingly like that of many osseous fishes, and illustrates the inex-
actness of the group of Ganoids, especially when internal anatomy is
not available for purposes of classification. The palato-pterygoid
arch, whose details seem so well brought out in the head of Platy-
somus, is not a little remarkable for the share it takes in the outer
configuration of the head. In fact, if the large cheek-plates of Trigla
are removed, the head of Platysomus is presented, with the single
exception of the maxilla, which is a narrow bar in place of the ex-
panded triangular plate of the fossil. If this plate is regarded as a
facial plate, and the maxilla restricted to the slender spatulate piece
marked off by a line near its lower margin, the peculiarity is not
less, since a suborbital attached to the maxilla and premaxilla (for
these two are closely united) is equally remarkable. The articulation
of the maxilla with the pterygoid plates is not quite certain—they
overlap and are closely related at least; but even their articulation
could not be regarded as wholly exceptional, since it only differs
from the similar arrangement in Crocodilia by the absence of an os
transversum. To Zrigla a further physiological resemblance may be
noted. The great size of the buccal cavity is obtained in both by
the same means, namely, the lateral extension of the palatine arcade,
and in both doubtless has reference to the predatory habits of the
animal. The head of Platysomus is narrow, but every available
space is secured for the mouth by the tenuity of the pterygoid appa-
ratus ; 1n fact, only the thickness of these bones is to be subtracted
from the transverse measurement to give the entire space available
for food. In Amphicentrum, on the other hand, the hard food, to
whose attrition the tubercle-teeth are adapted, required less space; or,
more correctly, required closer approximation of the crushing sur-
faces. Hence the broader jaws, low-set palate and contracted cavity,
though the gape is wider than in Platysomus. In this genus, there-
fore, the palato-pterygoid arcade recedes from the surface of the
head, and is concealed by a covering of skin, or possibly by the de-
velopment of membrane-bones. In no point is the difference of the
two genera more striking than in the maxilla; and the light which
that bone in Amphicentrum throws upon the anatomy of Pycnodus,
gives it peculiar interest. In Platysomus it is as in Paleoniscus and
other Lepidosteids—a single thin bone with small laniary teeth,

* The scale-ornament of P/. striatus manifests, in many specimens, a tendency
to the granular form. The figure substituted for that of this species in the

‘ Poiss. Fossiles,’ pl. 17, is accompanied by no description of the conical teeth
figured. In the meantime, therefore, it must remain among the Platysomt.

312 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Feb. 21,

contrasting, therefore, with the crushing-plates of Amphicentrum.
In Pycnodus, Thiolliére denies the existence of a maxillary, and finds
the analogue of the upper jaw in the palato-vomerine rows of crushing
teeth. Wagner had figured, but not identified, a triangular plate
whose forward attachment is in the premaxillary region. This,
Thiolliere regards as a suborbital only, it would seem, on the ground
that its overlapping the prominent lateral mandibular teeth presents
difficulties ; in his view, therefore, the palato-vomerines were naked. ©
Heckel* describes a specimen in which he finds a fragment of a
maxilla. It is to be supposed, therefore, that he regards this as
distinct from the bones bearing the superior mass of tritors. Am-
plicentrum gives the explanation of the arrangement: the outer
erest of the mandible is the higher of the two, and is external to
the inner maxillary crest, that, namely, which supports the denti-
cles. Doubtless the palatal plates were attached to the maxilla,
the latter having no free motion, as in most fish. Here, therefore,
the same difficulty is present as in Pycnodus; but the overlap of the
mandible by the labial flap of the maxilla is unquestionable. The
triangular plate in Pycnodus becomes, then, the simplest form of
maxilla, an edentulous mobile plate covering in the oral cavity late-
rally. In Amphicentrum, therefore, the overlap is greater in degree
than, but similar in kind to, that partially developed in Aechmodus,
Dapedius, and Tetragonolepis. From the Pyenodonts Amphicentrum
is separated by the absence of teeth in the premaxillary and preman-
dibular regions, which rather resemble beaks than the same parts in
ordinary fishest. ‘The smaller gape and coincident change in place
and direction of the opercular apparatus further separate them, as
will be seen from Thiolliére’s restoration (fig. 4), which I believe
to be correct, so far as the less perfect specimens in this country
enable me to judge. If to this be added the absence of a ventral fin
in Amphicentrum, and the less development of its vertebral arches,
the data seem sufficient to justify the reference of this genus to a
family distinct from, yet allied to, the Pycnodonts, and linking it
with the Lepidosteids.

Comparison with Achmodus, as the type of that group whose
association with the Pycnodonts Thiolliére justly condemns, shows a
divergence even more considerable than from Pycnodus, as will
appear from the restoration (fig. 3), and from the characters of the
teeth (Quart. Journ. Geol. Soc. vol. ix. p. 274, vol. x. p. 367). For
not only are the number and arrangement of the head-bones differ-
ent, but the structure and mode of articulation of the scales separate
this and allied genera from Pycnodus further than the latter is re-
moved in these points from Amphicentrum.

The Pycnodont affinities of Pl. macrurus=EHurysomus, mihi, being

* Sitzungsberichte der k.-k Akad. der Wissenschaften, Math.-nat. Classe,
vol. xii. 1854, p. 433.

+ The great height of the premaxillary ascending processes, relied on as evi-
dence of the mobility of the muzzle, is here associated with rigidity of the whole
oral structures, and even in Platysomus the constant connexion of premaxillaries
and maxillaries in dislocated examples suggests that in that genus also the pro-
trusion of. these parts was very limited.

PLATYSOMUS. : ole

1866. ] YOUNG

accepted on the authority of Sir. P. Egerton, enough has been said
to prove, as I think, not only the distinctness of that genus from any
of the flat fishes of the Coal, but also that, as yet at least, the family
to which it belongs has no true representative in the Carboniferous
series, .

-Mesorzpis, nov. gen. (Pl. XXI.)

Among a number of specimens marked Platysomi, three were found
on closer inspection to belong to a new genus. They are charac-
terized by the presence of a small ventral fin, a longer anal, and a.
dorsal which extends from opposite the anterior border of the former
to the posterior margin of the latter. The scales are broader in
proportion to their height than in Platysomus or Amphicentrum,
while the lepidopleura, weaker than in those genera, approach
somewhat to the kind of articulation present in Amblypterus and
Eurynotus. The imperfection of the head prevents anything being
said of it, save that the suprascapular is larger than in the above
genera, both it and the operculars rather resembling those of Hury-
notus, especially in the presence of concentric growth-lines. For-
tunately, however, one specimen shows three teeth, and these are
closely similar to those described by Sir P. Egerton in Pl. macrurus,
presenting a bluntly conical, minié-bullet-shaped crown with a con-
stricted neck, much like the Globulodus of Minster.

From the characters of the scales I propose the name Mesolepis
for this genus, and give the following definition :—

Body oval, or arched in the anterior dorsal region, terminating by
a blunt prolongation in the upper caudal lobe. Pectoral fin large,
its extremity rounded. Ventral small, narrow, at, or slightly in
front of, the middle of the body, equidistant between pectoral and anal.
Dorsal commencing opposite the ventral, and extending to the tail-
root, terminating opposite the posterior margin of the anal, which is
rather more than one-half its length. Caudal root strong; upper
lobe larger than lower. The anterior rays of all the fins are the
longest, and bifurcated only at their extremities; the following rays
are slender and divided so as to form a delicate fringe. Orbit large,
well forward, close to the facial line. ‘Teeth stalked, with a con-
stricted neck and smooth bluntly conical crown. Scales quadrila-
teral, those on the flanks higher than broad; the others more equi-
lateral. Ornament on them, and on head-bones, tuberculo-linear.

Two species are distinguished by the following characters :—

MS Wanor (Pl. xxi. figs. 1, 3).

Body ovate; the posterior dorsal slope more rapid than that of
the anal region. Length of trunk, from pectoral to tail-root, nearly
twice its greatest depth. Caudal root thick, elongate. Scales orna-
mented with tubercles, more or less confluent into approximately
vertical ridges.

M. scALARIs.

Body more arched dorsally. Tail-peduncle very short and slender.
VOL, XXII.— PART I. Vi

314 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 21,

The tubercles on the scales arranged in transverse close-set ridges
over the middle two-thirds of the scale; above and below the ridges,
irregular tubercles; and towards the posterior margin, sinuous
tubercular lines. The anterior border of the scale traversed by two
or three fine vertical striz. .

In general form of body this genus comes nearest to Amblypterus,
from which the size of the dorsal and anal fins, the character of the
ornament, and the proportional size of the scales, distinguish it.
From Hurynotus, the relatively larger head and scales, and the tuber-
cular ornament are equally marked grounds of separation, while the
teeth are in strong contrast with the small conical Lepidoid armature
of the jaw in that genus.

Both species have, as yet, occurred only in North Staffordshire ; but
the appearance of several fragments from other districts renders it
probable that the genus is not confined to the English coal-fields.

Evrynotus, Agassiz.

I have received, through the kindness of Sir P. G. Egerton, the
following remarks on this genus, in the form of extracts from letters
addressed to him by the late Hugh Miller, and gladly comply with
his wish for their publication :—

Edinburough, Feb. 3, 1849.

Max. DEAR Sry Se ieee I found, only a few weeks ago, a group
of palatal teeth of a rounded form, with a slight dimple in the centre
of each (which I used to set down as belonging to some Placoid),
existing as the palatal teeth of the Hurynotus crenatus of the Coal-

measures ...... ‘¢ Hues MILLER.

Edinburough, Feb. 17, 1849.
PEE Keh “I was desirous that in replying to your favour of the
6th inst. I should be able to send you with my communication a
cast of the specimen of Hurynotus crenatus, in which I detected the
palatal teeth referred to in my last. The cast which I now enclose
is a good one, and exhibits the rounded granules of the creature
scarce less distinctly than the original, one of the finest of this species
of Ichthyolite which I have yet seen, and which belongs to our Free
Church College Museum. The straightness of the line along the
back from the head to the point of the dorsal fin seems a striking
characteristic, and has, I think, in the general outline a rather
pleasing effect. At least, it would not be easy to construct a fish of
a breadth so great in proportion to its length, that would be equally
handsome, were this line different. Of the teeth, you will find some
eight or nine remaining immediately over what seems to be the
under jaw, and the rest represented by the little pit-hke sockets
which they occupied. The original specimen is from a limestone in
the neighbourhood of Crail, in Fife, identical in appearance and
character with the limestone of Burdie House.
“Tam, my dear Sir,
“ Very respectfully yours,
Sir Philip de M. Grey Egerton. “¢ Huen Minter.

18 66.] YOUNG——PLATYSOMUS. oh

Many specimens of this genus from the Fifeshire Carboniferous
rocks are in the Museum of St. Andrews, but the head in all these
specimens is imperfect. In the British Museum there is a specimen
which, in all save “the dimple,” might be that from which Miller’s
description was taken. The tritores and their sockets are well seen ;
not all are of equal breadth, some seeming of smaller diameter and
thinner root, a difference comparable to that seen among the teeth
of Pyenodonts. The teeth seem, as Miller has stated, undoubtedly
palatal, and, as such, disposed in several rows. The small opportu-
tunity I have had of studying Hurynotus, prevents me from doing
more than expressing my belief that the structure of the head agrees
with that of Mesolepis, the operculars being narrow and the supra-
scapulars elongate, as in that genus. The form and position of the
dorsal, ventral, and anal fins are also similar, while the nuchal line
to which Miller draws attention has the same characters in both
genera, and in others which are included under Lepidopleuride.
The external ornament of the scales differs wholly in kind; but to
this less weight is due than to the absence of the back-stays, which
linger in reduced dimensions on the anterior scales of Mesolepis.
That name was selected to express the transitional character of the
genus, and Hurynotus supplies the next step in the departure from
the Lepidopleurid type. Wherever, therefore, Mesolepis is placed,
there Hurynotus must also go. The cranial structure, traced through
the other genera of the suborder, cannot be demonstrated in these
two forms, but complete specimens would probably not depart far
from it. The dental characters seem decisive, and warrant the
juxtaposition of Mesolepis and Hurynotus as aberrant forms of the
Lepidoplewrde. Amblypterus, the genus they approach nearest in
shape, is widely separated from them by its dentitional characters,
which, as well as its cranial anatomy, place it among the Lepidos-
teide, not far from Oxygnathus. Nor is Lepidotus less distinct, as
appears from Quenstedt’s valuable memoir.

The five: genera just described form, with the family of Pycnodonts,
a natural group by which the Ganoid affinities of the latter are in-
creased, its Teleostean relations being at the same time brought into
greater prominence. The least variable common feature is the
structure of the scales, whence the name Lepidoplewride may be
given to the group, whose definition is as follows :—

Suborder LerrpoPLevRipz*.
Ganoids with heterocercal equilobate tails. Body rhomboidal,

* The word “ pleurolepida,” applied by Sir P. Egerton to the articular back-
rib of Pycnodont scales, has been altered to “‘lepidopleura,” partly to render the
term more descriptive, partly to secure euphony in the subordinal title. The
solid advantage which excuses the change is, that confusion is thereby avoided
between Lepidopleuride as above defined, and Pleurolepide as used by Quenstedt
(Handb. der Petrefactenkunde, p. 209). The latter name includes the Pyeno-
donts, and along with them Placodus, the group being stated to be intermediate
between Chondrostean and Holostean Ganoids, z.e. those on the one hand in
which scales and head-bones are the chief fossil remains, and those on the other

Zz 2

316 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 21,

covered with rhombic scales, articulated by strong ribs traversing
their anterior margin internally. Dorsal fin equal to half the length
of the trunk. Anal fin also with an elongate base. Ventrals, when
present, small. Paired fins non-lobate. Branchiostegal rays not
taking the form of broad plates. Notochord persistent. Arches
well ossified.

I. Ventral fin wanting.
PLATYSOMIDA.

Teeth uniserial, conical, sharp. Palate-bones edentulous.—Platy-
somus, Agassiz, partum.

AMPHICENTRID A.

“Dorsal and ventral margins sharply acuminated. ‘Teeth in the
form of tuberculated plates on the maxillary, mandibular, and palato-
vomerine bones. Premaxillary edentulous.—Amphicentrum, n. g.

EURYSOMIDA.

Teeth in the form of blunted cones, on a peduncle with a constric-
ted neck.—Hurysomus (=Platysomus, Agassiz, partim.).

Il. Ventral fin present.
MESOLEPID.

Teeth similar to those of Hurysomus.—Mesolepis, n. g.; Hurynotus,
Agassiz.

PyYcNODONTID A.

Teeth oval, hemispherical, or, if elongate, blunted cones.—Pycno-
dus, Mesodon, Gyrodus, &c., (except the Labroid forms of Cocchi).

The arrangement here sketched does not affect the question which
further research may raise as to the true position of the genera
included under it. The group is transitional between the Ganoids
and Teleosteans, and is equivalent to the suborders, 1. Amiade,
2. Lepidosteide, 3. Crossopterygide, 4. Chondrosteide, and 5.
Acanthodide. By Platysomus it approaches Paleoniscus and its
allies, while Pycnodus and Amphicentrum conduct to the Labroidet
and Sparoide:. From the Pycnodonts the above definition excludes
Tetragonolepis and its allies by the negative character of absence of
-lepidopleura, and by the important positive differences of cranial
structure already illustrated.

The restoration of ventral fins by Agassiz in the genus Platysomus
was a matter of inference, which perfect specimens have disproved.
His generalization as to the non-appearance of apodal fish prior to

in which parts of an osseous skeleton are more distinctly preserved. To the
former belong the Lepidoids, to the latter Thrissops, Macropoma, Leptolepis,—a
miscellaneous assemblage. This classification is artificial and inaccurate, its
basis—the amount of surviving structures—being only in appearance a zoological
one. The character selected to define and designate the subfamily occurs in
more genera than those included by Quenstedt under it.

.

KI PLEX §

h

ran

Quart.Jowrn Ceol Soe Vol.

C.R. Bone .del.etlith . M&li Hanhart mnp

23 iP EC ei ia ie

,
a
%

“Ouart Journ Ceol.Soc Vel SOUT Pl Rx

R.Bone del.et lth ' M&NHanhart mp

MESOLE PIS 6c bigac yO iio.

Seer

)

1866. | YOUNG—-RHIZODUS. 317

the Chalk, thus also falls to the ground. The absence of this mem-
ber cuts off Hurysomus from the Pycnodonts proper, which are thus
restricted to Mesozoic times ; for that family is clearly separated from
Eurynotus and Mesolepis by the form of the suprascapular bones, as
well as by the different position of the opercular plates, by the
structure of the scales, and by the absence of fulera on the upper
caudal lobe.

_ EXPLANATION OF PLATES XX. & XXI.
Puate XX.

. Amphicentrum granulosum, one-half the natural size.

. Maxilla of A. granuloswm, natural size.

. Mandible of A. granuloswm, seen from without.

The same seen from above.

Outer surface of a scale of A. granulosum, natural size.
. Inner surface of a scale of A. granulosum, natural size.
. Palatine armature of A. granuloswm, magnified.

Fig.

NID CUR Oo DO

Puate XX.

Fig. la. Mesolepis Wardi, natural size.
16. Outer surface of scales of M. Wardi, magnified.
lc. Inner surface of scales of M. Wardi, magnified.
2. Head of Platysomus parvulus, twice the natural size.
3. Teeth of Mesolepis Wardi, twice the natural size.

5. Note on the Scares of Ruizopus, Owen.
By Joun Youne, M.D., F.G.S.

[This paper was withdrawn by permission of the Council. ]
[ Abstract. ]

ATTENTION was drawn to the fact that, on a slab in the collection
of the Royal Society at Edinburgh, the characteristic Rhizodus teeth
occur along with thick. bony scales, whose exposed area is orna-
mented with coarse tubercles, usually irregularly disposed, while the
overlapped anterior area is concentrically striated. These characters
confirm the generic distinctness of Rhizodus from Holoptychius,

whose smooth anterior and rugose free surfaces contrast with those
described.

March 7, 1866.

Edward Filliter, Esq., Leeds; Myles Kennedy, Esq., Hill House,
Ulverston; and Lieut. Charles Warren, R.E., Gibraltar, were elected
Fellows.

Dr. Joseph Leidy of Philadelphia was elected a Foreign Member.

Prof. J. P. Lesley, of Philadelphia; and Prof. Reuss, of Vienna,
were elected Foreign Correspondents.

1

318 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,
The following communications were read :—

1. Documents relating to the Recent Votcanic DisrurBances in the
NurieHBournoop of Santorrno*.

[ Abstracts. ]

Tue document first received is a letter from Consul St. Vincent
Lloyd to the Rt. Hon. the Earl of Clarendon, dated Syra, February
8, 1866, in which he states that on or about the Ist of that month,
the sea in the neighbourhood of the Kaimeni islands, in the centre
of the great ancient crater forming the harbour of Santorino, began
to show signs of volcanic action ; the result was the formation of a
new island, which at the date of his report had become nearly joined
to the southern extremity of the island Nea Kaimeni. Consul Lloyd
also gave an account of the eruption, mentioning that it was ac-
companied by loud subterranean noises, flames of fire, and ebullition
of the sea. Slight shocks of earthquakes had been felt at Santorino,
where the inhabitants were much alarmed.

In a second letter to the Karl of Clarendon Mr. Lloyd encloses a
letter which he had received from Mr. A. Delenda, H.M. Consular
agent at Santorino, in which was given an account of the phenomena
attending the eruption as they were observed day by day at Nea
Kaimeni, from February Ist to February 7th inclusive. Mr. Delenda
particularly describes the boiling of the sea and the scattering
through it of coloured matter, as well as the appearance of flames,
the formation of pools of fresh water on Nea Kaimeni, the upheaval
of a new island, and the subsidence of some of the houses.

In a letter dated February 16th addressed to the Earl of Clarendon,
Mr. Erskine, British Minister at Athens, enclosed a copy of
‘La Grece’ newspaper of February 15th, containing letters from M.
Decigala dated 23rd, 24th, 25th and 26th, of January. From these
letters it appears that signs of volcanic action were observed at a
place called Voulcano as early as January 18th, and that the new

* These documents consist of the following Reports, the abstracts of which
are here printed together by Order of the Council :—

1. Report from St. Vincent Lloyd, Esq., H.M. Consul at Syra, to the Rt. Hon.
the Earl of Clarendon. Communicated by the Secretary of State for Foreign
Affairs. Read March 7, 1866.

2. Report from St. Vincent Lloyd, Esq., H.M. Consul at Syra, to the Rt. Hon.
the Earl of Clarendon, enclosing letters from A. Delenda, Esq., H.M. Consular
Agent at Santorino. Communicated by the Secretary of State for Foreign Af-
fairs. Read March 7, 1866.

3. Report from Morris Erskine, Esq., British Minister at Athens, to the Rt.
Hon. the Earl of Clarendon, enclosing letters from M. Décigala. Communicated
by the Secretary of State for Foreign Affairs. Read March 7, 1866.

4, Report from Commander G. Tryon, of H.M.S. ‘Surprise,’ to Vice-Admiral
Sir Robert Smart, K.C.B. Communicated by the Lords Commissioners of the
Admiralty. Read March 21, 1866.

5. Report from Commander L. Brine, of H.M. Steam-sloop ‘ Racer,’ to Vice-
Admiral Sir Robert Smart, K.C.B. Communicated by the Lords Commissioners
of the Admiralty. Read April 25, 1866.

6. Report from M. Fouqué to the Eparch of Santorino. Communicated by
Sir R. I. Murchison, Bart., K.C.B., &. Read April 25, 1866.

1866. ] VOLCANIC DISTURBANCES AT SANTORINO. 319

island first appeared in the form of a reef on the night of January
22nd. M. Decigala describes at length the same phenomena as Mr.
Delenda, especially mentioning that the sea was coloured white, like
milk, and the formation of several lakes of very pure fresh water.
He gave to the new island the name of ‘ George the first, and he
minutely describes the manner in which it was gradually enlarged,
until on January 25th it formed a promontory of the island Nea
Kaimeni,

Two letters dated Malta, February 22nd, from Commander G.
Tryon, of H.M.S.‘ Surprise,’ to Vice-Admiral Sir Robert Smart,
K.C.B., contain that officer’s report. The ‘Surprise’ reached San-
torino on February 16th, and on opening the island of Nea Kaimeni
a new island, named Aphroessa by the Greek Commissioners, was ob-
served to have arisen from a new crater situated about 150 fathoms
from the south point of Nea Kaimeni. This new island was upheaved
from a depth of 14 fathoms, and at that time was 100 yards long and
50 wide; but it was daily increasing in size. Its appearance was
very gradual ; it first appeared above water on February 13th, but
for two days previous it was only one fathom under water. The
small bay in Nea Kaimeni, known as Mineral Creek, had also been
the scene of volcanic action, and at the time of Comm. Tryon’s
visit, the creek was not only filled up, but a pile of lava was formed,
300 yards long by 200 broad, which had completely buried the
houses which were in its way ; and this new hill was then gradually
increasing at the rate of from 6 to 8 feet per diem each way. At
that time these two localities— Mineral Creek and the new island
Aphroessa,—about two-fifths of a mile apart, formed the vents of
the volcanic action. The south-eastern portion of Nea Kaimeni had,
however, sunk considerably, and was still sinking. No fluid lava
had appeared, the new formations having been apparently pushed
up from below and extended laterally as they got to the surface.
Commander Tryon was unable to discover that any circumstances
connected with the eruption, or that any of the materials upheaved,
differed from what had been observed in other parts of the world.

Commander Lindesay Brine, of H.M. Steam-sloop ‘ Racer,’ in a
letter to Sir Robert Smart, dated Malta, March 13th, reports that
active volcanic action is confined to.two vents, except that the ancient
crater of Nea Kaimeni, by the rents at its summit, and the steam
escaping at its sides, appears to be in communication with them.
The active volcano forming part of Nea Kaimeni had been raised
from 70 to 130 feet above the sea, and consists of an irregular mass
of scoriz, pumice, clinker, and solid basaltic lava, and was slowly
increasing in all directions by the addition of matter thrown from
the crater. Commander Brine also gives a detailed account of the
commencement and progress of the disturbances; but it does not
differ materially from other records, except that it draws a distinc-
tion between the first-formed vents, from which there had been true
eruptions, and the new island, from which there had been no erup-
tion, but incessant noise (caused by the detachment of blocks from
the sides), much steam, and clouds of smoke.

320 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 7,

Sir Roderick Murchison communicated the contents of a report
made by M. Fouqué, the envoy to Santorinoof the Academy of Sciences
of Paris, to the eparch of Santorino. M. Fouqué states that a
fissure had opened between the George Promontory and the new
island Aphroessa, and that the points of eruption are simply the
sites of the deepest holes in the line of rupture, and that the non-
existence of a true crater is owing to the small quantity of ejected
matter and the feebleness of the eruption. Owing to the recent
progress made in the study of volcanos, M. Fouqué is enabled
to state that the eruption of Nea Kaimeni never presented more than
a very moderate degree of intensity. M. St. Claire Deville has
shown that there exists a constant and certain relation between the
degree of intensity of a volcano in action and the nature of
the volatile elements vomited at its mouth; thus, in an eruption
of maximum intensity, the predominant volatile product is chloride
of sodium, accompanied by salts of soda and potash; an eruption of
the second order gives off hydrochloric acid and chloride of iron ; one
of the third degree, sulphuric acid and salts of ammonia; and of the
fourth, or most feeble phase, steam only, with carbonic acid and the
combustible gases. Applying this principle to Nea Kaimeni, it ap-
pears that the eruption never exceeded the third degree of intensity ;
and when it created the greatest.alarm it gave off only sulphuric
acid, steam, and combustible gases, or products of the third and fourth
orders of volcanic activity. M. Fouqué therefore agrees with other
observers in believing that the fears of the inhabitants of the islands
were very nearly unfounded.

2. On the CarBonrFEROUS SLATE (or Drevontan Rocks) and the Otp
Rep Sanpstone of Soutrm IRenanp and Norra Devon. By J.
Beets Juss, Ese., M.A., F.R.S., F.G.S.

Contents.

I. Introduction. and the Cork and Midleton

II.

Sketch of the Upper Paleozoic
Rocks of the Southern portion
of Ireland.

Troughs.

7. The Knockadoon and Sheeps

Head Anticlinal, and the coun-

1. Wexford. try to the south of it.
a. Red Sandstones and Con- 8. Old Head of Kinsale.
glomerates in the Lower | 9. Cape Clear and Mizen Head An-
Silurian rocks. ae 3 ticlinals.
2. Hook Head. 10. The Bantry Bay Trough.
3. Waterford. 11. The Berehaven Promontory, and
4. Extent of the Old Red Sand- that of Iveragh and Dunkerron.
stone north and west of Water- | 12. Dingle Beds.
ford. 13. Gradual changes in the Litholo-

. Old Red Sandstone of North

. The Lower Limestone Shale of

a. The Kiltorcan Section.
6. The Comeragh Mountains.

Cork, South’ Waterford, and |
South Kerry.

the Youghal and Ardmore, |

gical character of the Old Red
Sandstone.

. General Conclusions on the Rocks

of the South-west of Ireland.

. Sudden Changes from thick lime-

stone to mechanically formed
rocks.

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 32]

III. Geological Structure of North 9. Probable Existence of a great Hast

Devon. and West Fault, with downthrow
1. Baggy Point to Dulverton. to the Northward.
2. Dulverton. 10. Thickness of the Rocks of North
3. Dulverton to Dunster. Devon on the ordinary hypo-
4. Dunster to Lynton. thesis.
5. Lynton and its neighbourhood. 11. Objections considered.
6. Lynton to Ilfracombe. 12. Considerations on the Devonian
7. Pickwell Down and Mortehoe. Fossils.
8. Aspect of the country. IV. Appendix.

I. Inrropvction.

Havine been able during the last summer to extend a little my
knowledge of North Devon, especially in the neighbourhood of Lyn-
ton, and having, as the result of my observations, become quite con-
vinced that the rocks of North Devon belong partly to the group
called Carboniferous Slate in Ireland, and partly to the Old Red Sand-
stone, I propose to lay before the Society the grounds of that con-
viction.

As I shall have to maintain that all the first geologists of the day,
including Professor Sedgwick, Sir R. I. Murchison, Mr. Weaver, Sir
HH. De la Beche and Professor Phillips have misunderstood the
structure of the country, let me hasten to avow my belief that no-
body whose observations were confined to Devon and Somerset, could
have arrived at any other than their conclusions. I fully admit that
the rocks near Lynton appear to be the lowest, and that there appears
to be a regular ascending succession of rock-groups from Lynton to
the latitude of Barnstaple. I am, however, compelled to dispute the
reality of this apparent order of succession, and to suppose that there
is, either a concealed anticlinal with an inversion to the north, or,
what I believe to be much more probable, a concealed fault running
nearly east and west through the centre of North Devon with a large
downthrow to the north, and that the Lynton beds are on the same
general horizon as those of Baggy Point and Marwood. As my
reasons for this supposition are derived from the experience acquired
during many years’ labour in the south-west of Ireland, I must in
the first instance endeavour to state the result of those labours in as
brief a form as possible.

It was at the close of the year 1850 that I succeeded my friend,
Dr. Oldham, in the Local Directorship of the Irish branch of H.M.
Geological Survey, when it was just entering on the examination of
the district alluded to. During many succeeding years the rocks
were patiently laid down on the six-inch Ordnance Maps by my
colleagues, Mr. W. L. Willson (now of the Indian Survey), Mr.
Andrew Wyley (who afterwards undertook the Geological Survey of
the Cape Colony), and Mr. G. VY. Du Noyer (now the senior Geologist
in Ireland). Sir H. De la Beche and Professor Edward Forbes fre-
quently gave their assistance to the work during those years. Sub-
sequently our force was strengthened by the addition of Messrs. G. H.
Kinahan, F. J, Foot, and Jos. O’Kelly, who still remain with us, and
Mr. A. B. Wynne, who afterwards left us for India. All those gen-
tlemen assisted in the examination of the district, and Mr. Salter

322 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

(after the death of Professor Ed. Forbes) spent part of one summer
In examining our fossils and visiting with me the principal fossil
localities. The fossils were collected by the late James Flanagan in
the first instance, and additions have been made by our present
collectors Charles Galvan and Alexander McHenry; and some of the
localities have been visited by Mr. W. H. Baily, who since the year
1857 has acted as Paleeontologist to the Irish branch of the Survey.
When I speak of the labours of the Survey, then, it is to those of the
gentlemen named I more particularly refer; my own share being
limited to general inspection of the work and comparison of the
structure of different parts of the district, together with laying down
the rocks of two or three small areas which happened to be typical
localities. |

I must not omit to mention that in our examination of this dis-
trict we had of course been preceded by Sir R. I. Griffith, and that
our more exhaustive operations only confirmed the general conclu-
sions which he had previously arrived at, as shown in the later
editions of his map. His name “ Carboniferous Slate” is perfectly
applicable to the grey slates and grits of the south-west of Cork, and
has accordingly been adopted by us ; and his boundaries agree gene-
rally with ours, except in one area where he takes a different base for
the Old Red Sandstone, and so far as the imperfect map on which
his results are published can be compared with the new ordnance
one-inch sheets.

I will now give a sketch of the Old Red Sandstone and Carboni-
ferous formations of the south of Ireland, commencing with the
County Wexford and following them to the western bays and head-
lands of County Cork*. |

Il. Sxetcu oF THE Upper Patmozoic Rocks oF THE SOUTHERN
PORTION OF IRELAND.

1. Wexford.—The Forth Mountain district, in the county of
Wexford, shows green and purple slates and grits, with large bands
of quartz-rock, which are believed to be part of the Cambrian for-
mation. The town of Wexford is built on these rocks. About a
mile to the north of it, however, there are several quarries in a red
sandstone and conglomerate just like some of the Old Red Sand-
stone of South Wales, dipping gently to the east and south-east, in
which direction a few exposures of Carboniferous Limestone were
obscurely seen. About a mile to the south of Wexford there are
several considerable quarries in dark-grey, compact or crystalline
limestone, with beds of black shale, from which a number of common
Carboniferous fossils were collected. In the townland of Kerloge,
near the old church, and not far from St. James’s Well, the lowest
beds visible of this limestone are full of pebbles of quartz-rock, a
crag of which, in situ (a part of the Cambrian formation), rises on

* Although much of the matter of this sketch may have been published before
_ in separate forms, I am not aware of any previously published-connected sketch
of the gradual but great change which takes place in these rocks as they are
traced across the south of Ireland.

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 323

the other side of the road. This Cambrian crag evidently stood asa
rock in the Carboniferous sea, and pebbles derived from it were em-
bedded in the limestone formed in that sea, and if there be any Old
Ked Sandstone about it, it is overlapped and concealed by the lime-
stone. A mile farther to the south-west, however, about Latimers
Town, there appears to be a district of red and yellow sandstone and
conglomerate interposed between the Cambrian ground and that in
which the limestone is found. A little farther on, quarries in red
and yellow sandstone occur, and a regular band of red and yellow
sandstone and conglomerate then runs to the south-west until it
terminates on the sea-coast. The best section may be seen at Dun-
cormick, about twelve miles south-west of Wexford, of which fig. 1

Fig. 1.—Section at Duncormick.
§8.B. Seafield House. Duncormick. N.W.

| |

a

ec
Length of Section, three-quarters of a mile.

Carboniferous Limestone. c. Old Red Sandstone. a. Cambrian rocks.

is a sketch. Several quarries were opened here in a dark-grey flaggy
and shaly limestone, very fossiliferous and highly fetid, which dipped
to the south-east at 25°. These lay between Seafield and Duncor-
mick, which latter village stands on red flaggy sandstones and red
shales, underneath which are yellow sandstones and conglomerates,
all dipping south-east at 25°. These beds are well exposed in the
village and road. North-west of the village, on the other side of the
road, green grits and slates, such as are seen everywhere in the Cam-
brian rocks of the Forth Barony, rise to the surface, undulating in
different directions and at various angles. The thickness of the
yellow and red rocks here is about 200 feet, while the limestone beds
must have a total thickness of 600 or 700 feet, if the dip of the beds
is the same in the concealed parts between the quarries, as itis where
they are open. We have taken the beds of red and yellow sandstone
and conglomerate thus described, for Old Red Sandstone. There are,
however, other beds of similar red sandstones and conglomerates to
be found to the south-east of this band, interstratified with the Car-

-boniferous Limestone, and therefore certainly not true Old Red Sand-

stone. This is a circumstance which occurs also in the northern por-
tion of Ireland, as also I believe in parts of England, so that the
mere occurence of red sandstones and conglomerates beneath some
beds of Carboniferous Limestone is not sufficient to entitle them to
be considered really Old Red Sandstone.

a. Red Sandstones and Conglomerates in the Lower Silurian Rocks.
—Thick masses of red shale and red sandstones and conglomerates
are interstratified also with the Lower Silurian rocks of Wexford
near Tagoat, and Waterford near Bunmahon. Those of Bunmahon
were at first presumed to be Old Red Sandstone let in by faults

324 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

against the Lower Silurian rocks; but having seen those near Tagoat
to be certainly in the Lower Silurian formation, I doubted the cor-
rectness of the supposition adopted at Bunmahon, and a recent
reexamination of the county by Mr. Du Noyer has shown these also
to be really Lower Silurian red sandstones and conglomerates. (See
Explanation of sheets 167 &c., of Irish Maps.)

2. Hook Head.—The Upper Paleozoic rocks which strike into the
sea south of Duncormick reappear on the coast, in the promontory
of Hook Head, partly in consequence of a change in the strike of the
beds, which there dip nearly due south, and partly from the land pro-
jecting farther to the south, as we proceed westwards. Fig. 2 will
give an idea of the lie and position of the Carboniferous Limestone
and undoubted Old Red Sandstone here; the latter reposing on
slates and grits which belong to the Lower Silurian group, as is
evidenced by their fossil contents at Duncannon Fort and else-

-where*. ‘These Lower Silurian beds are greatly contorted, as is
shown in the cliffs of Waterford Harbour for several miles. —

The Old Red Sandstone rests on the edges of these contorted beds
quite unconformably, as is shown in section fig. 2, and dips from

Fig. 2.—Section of part of Hook Head.

Coast
Templeton Harry-" Guard Lumsden

Church. lock. Station. Bay.
Ihe : {

+
neo Ss
Nit

Nessa

6

aoe : d*, Grey often flaggy limestone.
fe Cee aegis nian one {or Black shale highly fossiliferous.

A: Old Red Sandstone: jae and yellow sandstones and shales above.

Red sandstones and conglomerates below.
Be La wer Suku. One shales, slates, and fine-grained grey
grits.

them to the south, as a whole, but is itself undulated at slight angles
and broken by faults probably of small throws. It is well shown in
cliffs about 40 feet high for about a mile and a quarter along the
shore of Waterford Harbour and for nearly two miles along the
eastern shore of the promontory, which does not cut so directly across
the strike of the beds as the western shore does.

The thickness of the Old Red Sandstone here is not exactly
determinable, owing to its disturbed “lie,” but it must be at least
six or seven hundred feet. The lower beds consist of red sandstones
and red shales, with beds of red conglomerate occasionally. Higher
up the conglomerates become more massive, and beds of white con-
elomerate occasionally appear among the red. About the middle of

* See the list of Fossils and the Paleontological Notes by Mr. W. H. Baily
in the “ Explanation of sheets 169 &c. of the Irish Maps in the Memoirs of the

Geological Survey.”

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 320

the mass fragments of plant-stems occur, either as impressions on
the sandstones, or as flattened stems with a thin coating of coaly
matter. Little seams also of carbonaceous matter sometimes appear
between the beds.

Beds of greenish shale set in near the top of the Old Red Sand-
stone, the uppermost one being capped by a bed of grey “ fucoid ”
shale, which is taken as the base of the Lower Limestone Shale.
There are, however, here not more than from 10 to 20 feet of actual
black shale before we come up to the compact grey limestone. The
limestone beds are well shown in the low cliff on both sides of the
promontory as far as the extremity of the Head, a distance of two
miles and ahalf. They are much bent and broken, dipping in vari-
ous directions, although never at angles exceeding 30°, and rarely
above 10° or 15°. There is a belt of magnesian limestone (one of
the many places in which the Carboniferous Limestone is dolomi-
tised) about 400 yards wide, crossing the promontory before reaching
the extremity of the Head; but except in that space, the cliffs are
crowded with fossils, all of them of species which are known to occur
in the Carboniferous limestone elsewhere, as will be seen on refer-
ring to the lists by Mr. W. H. Baily, given in the Explanation of the
Sheet 167, d&c., of the Maps of the Geological Survey of Ireland.

3. Waterford.—Opposite the Hook Point, on the western coast
of Waterford Harbour about Dunmore, the Old Red Sandstone
spreadsin a nearly horizontal position over an isolated area six or
seven miles long by about two broad, resting unconformably on
Lower Silurian rocks, which rise steeply out from underneath it on
the west and north.

Two or three other isolated patches of similar size lie, like cakes
of Old Red, on the highly inclined Silurians on both sides of the
harbour further north, andin the southern angle of County Kilkenny,
between the rivers Suir and Barrow. .

These isolated patches are obviously pieces spared by the denu--
dation that has removed the rest, and uncovered the Silurian rocks
aroundthem. ‘They serve to connect the Old Red Sandstone of Hook
with the persistent mass of it which takes the ground north of the
eity of Waterford.

Immediately to the north-west of the city of Waterford, on the
south side of the river Suir, are some black slates, in which Diplo-
grapsus pristis and Graptolithus tenms are abundant. They dip north-
west at 60° and 70°. On the northern side of the river the slates
and grits of the Lower Silurian formation are of a greener hue and
more siliceous appearance, and are unfossiliferous, but dip in the same
direction, at 70° or 80°.

These beds are well shown in the cuttings in the cliffs at the back
of the houses by the railway station ; and on their upturned edges
lie great beds of brewn and red quartzose conglomerate, dipping north-
west at 10° or 15°.

These are the basal beds of the Old Red Sandstone; which may be
followed in one direction to the river-bank, on the other side of which
they reappear striking to the west into County Waterford; while in

326 - PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

the other direction they may be followed up the cliff to Mount Misery,
and for some miles to the north-east in County Kilkenny.

Above the conglomerates come red sandstones often flaggy and
and sometimes traversed by a rude slaty cleavage. These beds all
dip north or north-west at low angles towards some lower ground,
where a few scattered quarries show beds of yellow sandstone and
flag with yellowish or greenish shaly or slaty partings.

Fig 3. Section from Dunkitt House to Mount Misery, Waterford.

Dunkitt Mount
House Misery.
NW. | 4 Bee
Weary Ss
pr en a 2 i a 2 Ul “ail mm i}
))[- MM a a = a y a = im Saif mmm
at Cc b

Length of Section, about 2 miles.

d*, Grey crinoidal limestone in thick beds.
d. Carboniferous limestone. , d!. Dark-grey fossiliferous shales with flagey lime-
stones above and flaggy sandstones below.

Yellow and red sandstone above, red sandstones
ee ae and slates and red conglomerates below.
b. Lower Silurian. Grey, black, and greenish-grey slates and grits.

On Mount Misery there is not such a good exhibition of slaty
cleavage in the Old Red Sandstone as occurs in the finer sandstones
two miles to the west of Waterford, in the townland of Knockhouse
Upper. ‘The red sandstones which lie there between the coarse con-
glomerates, all dipping north-west at 20°, are traversed by a clea-
vage which, according to Mr. Du Noyer’s notes, dips north-north-west
at an angle of 50°, making them a rough sandy slate.

North of the slope of Mount Misery the ground is very low and
flat and little rock is shown in it except on the shores of the river Suir
at low water, where, immediately above the topmost bed of fine-
grained yellow sandstone are seen beds of grey earthy and sandy
shale, hard but brittle, weathering to a light-brown colour, with
partings of clayey shale in which marine fossils are abundant.

Mr. Salter, when he visited this locality with me, noted the occur-
ence of stems and other fragments of Rhodocrinus, and shells of the
genus Nucula (Ctenodonta) and Aviculopecten in the beds immedi-
ately above the yellow sandstones. Over these come light-yellowish
earthy friable shales, with seams of hard dark-grey caleareo-ferru-
ginous shale, and, above these, dark-grey shales with hard thin
nodular crystalline limestones all full of fossils. Above these are
dark-grey thin-bedded limestones, getting thicker, lighter in colour,
and more crystalline as we ascend. Large quarries are opened at
Granny and Dunkitt in these thicker crinoidal limestones; and nothing
but limestone, sometimes becoming suddenly magnesian, is seen for
three or four miles to the north of the quarries. (See section, fig. 3.)
In the shales which intervene between the massive limestones and
the yellow sandstones which form the top of the Old Red,
Mr. Salter noted the following fossils when with me on the occasion

~

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 327

above referred to, Poteriocrinus crassus, Actinocrinus polydactylus, a
species of Platycrinus and Pentremites; Corals of the genera Mich-
elinia, Zaphrentis, and Syringopora ; and the following shells; Orthis
filiaria, O. crenistria, Spirifera disjuncta, S. glabra, Athyris squa-
mosa, Strophomena analoga, Producta Martini, and a species of Pi-
leopsis (Acroculia).

4, Hatent of the Old Red Sandstone, north and west of Waterford.
—The Old Red Sandstone of Waterford just described extends con-
tinuously northwards into Kilkenny, and westwards through the
counties Waterford and Tipperary into Cork and Kerry. Following
it northwards to Kiltorcan and Thomastown it retains the same
general character as near Waterford, but a few miles north of
Thomastown, it gradually thins out, and finally dies away near Gores-
bridge (see Explanation of sheets 147 and 157 of Irish Maps) ; and the
Carboniferous Limestone then reposes directly on the Lower Silurian
slates and the Granite of the County Carlow.

a. The Kiltorcan Section.—At Kiltorcan, near Ballyhale, which is a
village about five miles south by west of Thomastown, in the Parish of
Knocktopher, are the quarries which have become celebrated for the
fossils discovered in them. For a full account of the geology of the
neighbourhood I must refer to the Explanation of sheets 147 and
157 of the Irish Maps in the Memoirs of the survey ; but will give
here the following brief summary of it :—

The Old Red Sandstone lies at a very low angle, the lower - beds
gradually rising towards the east into some brown arid moorlands,
one of the highest points of which is in the townland of Coolroe-beg,
785 feet above the sea. This conglomerate forms a little escarp-
ment there overlooking the valley of the Arrigle brook, which runs
northwards into the Nore below Thomastown.

Lower Silurian slates and grits, partly altered into mica-schist, and
Granite with highly crystalline greenstone, also probably of Lower
Silurian age and altered by the Granite, appear from under the base
of this Old Red Sandstone on the east, while towards the west it
dips gently to the village of Ballyhale, where it is covered by black
shales, and those again by grey limestone, as near Waterford *.

About half-way between Coolroe and Ballyhale some quarries
were opened at Kiltorcan in a greenish grey flag, interstratified with
brown sandstones and bright red slates. This greenish flag was

luckily not affected by the slaty cleavage, and when our fossil-col-

lector, the late James Flanagan, was assisting Mr. Wyley in the
examination of the district, he discovered some large. ferns and
bivalve shells there. This was in the year 1851, when the late
Professor Edward Forbes was with me near Cork, and we immediately
inspected the district together. Forbes afterwards named the shell
Anodonta Jukesii+ and the fern Cyclopteris Hibernica; but M. Adolphe

* The north-west boundary of the Granite under the Old Red cannot be
seen in this locality, and its place therefore is a little uncertain.

+ There is much inconvenience attending this practice of affixing personal
appellations to species of fossils. I can never speak or write of this shell without
feeling guilty of egotism, and conscious of the appearance of a wish to thrust it
into importance, because it has my own name attached to it.

— *

[ Mar. 7,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

328

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1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 329

Brongniart has since referred the latter to the genus Adiantites.
This quarry has been repeatedly visited since, especially by Mr. W.
H. Baily, and our present fossil-collectors C. Galvan and Alexander
M‘Henry, and, among other things, numerous scales and some teeth
of fish have been found. Many of these scales were decided by Mr. .
W. H. Baily to be those of Coccosteus, a determination in which
Professor Huxley, when he examined them, fully agreed; others,
respecting which the latter gentleman felt some doubt, are believed
by Mr. W.H. Baily to belong to the genera Asterolepis, Bothriolepis,
Glyptolepis, and Pterichthys, or certainly to be identical with those
figured by Agassiz under those names (see for figures Explanation _
of sheets 147 and 157 of Irish Geological Survey Maps). ‘There is
also part of the shell with a piece of the claw of a crustacean,
apparently a Hurypterus, among the fossils from these beds. We
have found the Anodon and the fern at other localities in Ireland,
as near Cork and at Toe Head on the south coast, in places where
the rocks were not so luckily preserved from cleavage as at Kiltorcan,
so that only a few fragments could be collected in a sufficient state
for transmission to the Museum*,

b. The Comeragh Mountains.—It was just now said that the Old
Red Sandstone of Waterford was not only continuous northwards to
Kiltorcan but westwards through Waterford and Tipperary. .

The ridge of Old Red Sandstone, shown in fig. 3. p. 326, may be fol-
lowed along the south side of the valley of the Suir for 25 miles to the
westward, as far as the neighbourhood of Clonmel, the height of the
ridge increasing to an altitude of 600 and 800 feet, and the dip of
the beds to 50° and 60°, and occasionally more.

The Old Red Sandstone rests unconformably on Lower Silurian
rocks, which for the first 20 miles are exposed in the country to the
south of it, and dips northwards conformably under the Lower
Limestone shale and Carboniferous Limestone, as it does at
Waterford. About five miles, however, before coming’ to Clonmel the
Old Red Sandstone, after rising steeply out from underneath the
limestone valley in order to form this ridge, is no longer denuded
towards the south so as to expose the Lower Silurian base on which
it rests, but has been left as a cover to those beds. Doubtless this
cover formerly extended over the whole of the Lower Silurian area.
In the part where it is still preserved, the lower conglomerate of the
Old Red, after rising up at angles of 50° or 60°, gradually flattens
towards the south, and ultimately becones horizontal, or undulating
gently at angles of 10° or 15° for a space of about twelve miles, and
forms the base of a mass of high ground called the Comeragh Mount-
ains. These are upwards of 2000 feet high, the highest point being
2597 feet above the sea. They end in steep indented escarpments
towards the east, in which the beds are thoroughly exposed.” One
precipice over Lough Coumshingaun is itself 1250 feet in height,
exposing horizontal beds of Old Red Sandstone through the whole
height. To the south of the Comeraghs the beds dip steeply again

* Mr. Doran, the fossil-collector, also discovered a fine specimen of the Anodon
in the Old Red Sandstone near Clonmel.

VOL. XXII. PART I. ; 2A

330 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

to the south, and the surface of the ground also falls again in that
direction, but much more gently. The Old Red then passes beneath
the Lower Limestone shale and Carboniferous limestone of the valley
of Dungarvan, as shown in Fig. 5.

The thickness of this Old Red Sandstone is, according to Mr. Du
Noyer, not less than 1700 feet near the Suir valley, increasing towards
the south-west untilit becomes upwards of 3000 feet north of Dungar-
van (see Explanation of sheets 167 &c. of the Irish Survey Maps, and
the Longitudinal section, sheet 13). The Lower Limestone shale also
is materially thicker on the south of the Comeraghs than it is on the
north. The black shales and the flaggy limestones near Clonea Castle,
about four miles east of Dungarvan, seem, from their exposure on
the shore, to have a thickness of 600 or 700 feet. They, however,
as well as the limestones immediately above them, are so much
affected by slaty cleavage that the bedding is often greatly obscured
by it. This fact is observed by Sir H. De la Beche in the ‘ Memoirs
of the Geological Survey,’ vol. 1. p. 76.

The gently undulating arch of Old Red Sandstone which forms the
Comeragh Mountains, is continuous as a ridge of lofty ground for
thirty-five miles to the westward, first sinking to 650 feet in the
pass of Ballynamult, then rising to 2600 feet in the peaked hills
called the Knockmeildown Mountains, and then dying away in the
much lower Kilworth Hills south of Mitchellstown. The gentle un-
dulations in the beds in the Comeraghs become more pronounced
farther west, and the beds are folded into sharp anticlinal and syn-
clinal curves, which let in a little trough of shale and limestone in
the very centre of the hills between the Knockmeildowns and the
Kalworth Hills.

The axes* of these curves then gradually sink towards the west,
and the Old Red Sandstone dissappears in that direction beneath the
plain of Carboniferous Limestone that extends from Mitchellstown to
Mallow. The undulations in the beds, however, do not cease, the
limestone beneath the plain being bent into curves like the Old
Red Sandstone of the hills.

This Carboniferous Limestone, after wrapping round the extremi-
ties of the Kilworth Hills, runs down the valley of the Blackwater
past Lismore and Cappoquin, and is continuous out to Dungarvan
Harbour and Clonea. Between Fermoy and Dungarvan the Lime-
stone lies in a long narrow trough, the Old Red Sandstone, which
dips underneath it from the hills on the north, quickly rising out
again towards the south into a persistent ridge, which stretches east
and west right across this part of Ireland from Dungarvan Harbour
to Doulus Head in Dingle Bay, a distance of 120 miles.

5. Old Red Sandstone of North Cork, South Waterford, and South
Kerry:—This continuous ridge forms the northern margin of a tract
of Old Red Sandstone, having a mean length of 100 miles. It is
18 miles broad at the eastern end, measuring from a little south of

* By the axis of a curve I understand the purely imaginary line about which
the beds may be supposed to be bent, and not any particular mass of rock that
appears at the surface.

1866.] JUKES—OLD RED SANDSTONE AND DEVONIAN. dol

Lismore to Knockadoon Head on the south side of Youghal Bay, and
spreads to a breadth of 36 miles towards its western extremity, mea-
suring from Rossbehy in Dingle Bay to Sheeps Head on the south
side of Bantry Bay. Its southern as well as its northern margin is
formed by a continuous ridge of Old Red Sandstone, stretching across
Ireland from sea to sea, forming Sheeps:Head on the west and Knocka-
doon Head on the east, the distance between them being nearly 90 .
miles. This large area of Old Red Sandstone is puckered into nume-
rous anticlinal and synclinal curves, the axes of which run nearly
east and west in its eastern portion, but bend to west-south-west and
east-north-east on its western side. These axes also rise and fall
frequently along their course, the lower beds rising out to the surface
where each axis rises, the higher beds taking the ground where the
axis falls. Not only do different beds of Old Red Sandstone crop
up, then, as we trace the summit of an anticlinal curve, or take the
eround as we follow the hollow of a synclinal trough, but in the
latter case the Carboniferous Limestone is often brought in below
the present surface of the ground, and preserved as a limestone
trough. These limestone troughs run sometimes for many miles,
until the gradual rise of the axis of each synclinal brings the lowest
limestone beds to the surface, and in its prolongation the synclinal
curve is traceable only in the Old Red Sandstone.

Towards the East we have first the limestone trough of Rath-
cormack, Tallow, and Aglish, about 24 miles long; secondly the
small trough of Clashmore, only two miles long. Both these seem to
terminate eastwardly in faults which jump the Old Red Sandstone
up above the level of the limestone in the same line of strike.
Thirdly we have the trough of Youghal and Ardmore, about 10 miles
long; fourthly comes the long trough of Midleton and Cork, which
runs westwardly from Youghal Bay to Cookstown, a distance of
55 miles*. North of the extremity of this are the minor Carboni-
ferous troughs of Rwerstown, Blarney, Ardrum, Coachford, and
Annaghallagh (the latter a little south-west of the town of Macroom),
all nearly on the strike of the Ardmore and Youghal trough. To
the west of the Annahgallagh trough the undulations do not bring
in any beds superior to the Old Red Sandstone itself, for a length
and width of upwards of 20 miles between Dunmanway and Mill-
street. A great thickness of Old Red Sandstone is exposed in this
tract, as the beds in some places dip steadily north or south at
angles of 50° or 60° for two or three miles continuously, clear
exposures of them being observable on the sides of barren hills bare
of drift. These sections show a thickness of 5000 or 6000 feet in
the body of the formation, without reaching either the uppermost
or the lowermost beds, and such sections are of no unfrequent

* In a hasty traverse of the country about Pembroke and Tenby, I was struck
by the great similarity both in the physical geography and geology of that country
to that of the Cork and Youghal district. Mr. Salter, in his paper “On the
Upper Old Red Sandstone and Upper Devonian rocks,” notices the identity of
the beds of Pembrokeshire and South Ireland (Quart. Journ. Geol. Soc. vol. xix.

-p. 474 et seq).
2AZ

352 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. i

occurrence. Farther west we again get Carboniferous beds in the
hollows of two of the synclinals, making first the Trough of Kenmare
with ordinary Carboniferous Limestone for about 10 miles, and
Carboniferous Slate only for about 12 or 15 more. This is nearly
in the strike of the Tallow trough. Secondly comes the Bantry
Trough, which contains Carboniferous Slate only, and is about 40
miles long, being extended 4 or 5 miles farther to the east than it
otherwise would be, in consequence of the ground rising in Shehy
Mountain to a greater height than it usually does when it is formed
of Carboniferous rocks. This is in the strike of the Cork and
Midleton trough.

The two Carboniferous troughs of Kenmare and Bantry have been
eroded on the west into two beautiful bays, separated from each
other by a lofty Old Red Sandstone ridge, of which whe highest point
(Hungry Hill) is 2250 feet above the sea.

Kenmare Bay is separated from Dingle Bay i another broader
and loftier promontory—that of Iveragh and Dunkerron, in which
Carrantuohill (38414 feet) and Macgillicuddy’s Reeks lie.

The rocks are well shown in both these promontories in nume-
rous glens and ravines as well as upon bare hill-sides, and while
they often undulate in sharp and frequent curves, especially near
the centres of the districts, there are also numerous places where a
steady dip of 60° either to the north or south may be observed for two
or three miles; and this in places where the majority of the rocks
are hard massive sandstones with thin interstratified slates, so that
no mistake can be made of cleavage, or oblique lamination, for true
bedding. Notwithstanding the great depths to which we can thus
penetrate into those beds, there is no appearance of any change in
the nature or “lie” of the rocks which would enable us to draw
a lower boundary to them, or allow us to suppose that we have
reached another lower formation.

The rocks consist of red, purple, brown, and greenish sandstones,
sometimes becoming purplish- -grey, but never black or dark-grey,
and they are variously interstratified with bright-red, purple, lilac,
greenish, and yellowish clay-slates. The slates occasionally pre-
dominate to such an extent as to cause the mass to assume the
character of a great clay-slate formation, the transverse cleavage
cutting across the beds generally at a high angle and with a steady
strike of west-south-west and east-north-east, but dipping sometimes
to one side and sometimes to the other side ‘of their strike. Thin
bands of slate between thick grits are often perfectly cleaved, the
cleavage affecting the grits to such an extent as to make them break
into sharp dog-toothed indentations at top and bottom, and some-
times to split readily into thin flags at right angles to the bedding.

Although the districts formed of this Old Red Sandstone have
been twice diligently searched by our fossil-collectors (James Fla-
nagan and Charles Galvan) as well as by the gentlemen who laid
down the rocks upon our maps, and have been examined by many
other independent observers, no trace of a fossil has, as yet, rewarded
the search in either of these two promontories, except some frag-

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 333

ments of plants in the uppermost beds, and some very obscure
impressions that might be those of plants lower down in the beds
near the Lakes of Killarney.

A curious track, also, in some purple slates near Valencia Island,
was discovered by Mr. Kinahan. It seems to be such a row of
minute indentations as might be made by the claws of some
Crustacean. (See Explanation of Sheet 182, &., p. 11.)

The uppermost part of this great series of reddish and brownish
rocks is more brightly and variously coloured than the lower portion ;
lilac-coloured slates occurring there more frequently than elsewhere,
while the peculiar kind of massive sandstone, which acquired the
name of Glengarriff Grit with us, is more abundant lower down.
The yellow sandstones and greenish slates which characterize’ the
top of the Old Red in Waterford pass into harder and slatier grits
further west, and purple slates make a greater figure among them ;
though these are by no means absent to the eastward, as may be
seen in the hills south of Clonmel. Throughout the whole region,
from the south side of Dungarvan Harbour to the extremities of the
peninsulas south of Dingle Bay, there is hardly a trace of conglo-
merate in this Old Red Sandstone, the whole being essentially a
' clay-slate formation, with great groups of sandstone distributed
through it.

6. Lhe Lower Limestone Shale of the Youghal and Ardmore, and
the Cork and Midleton Troughs.—In fig. 5 and its explanation it is
shown that the lowest margin of the Carboniferous Limestone and
the top of the Old Red Sandstone are thicker at Clonea than at
Waterford. A still greater development of these shales and the
sandstones associated with them is apparent in the sections about
Ardmore* and Whiting Bay, and near Youghal.

In the quarries immediately north of the latter town the thick
dark-grey and brown sandstones are well shown, some of them
haying rippled surfaces, others showing impressions of large plants
several inches across. Many of these beds were originally calca-
reous, and now are externally converted into rotten-stone. The
dip in this locality is 70° north, and the group of shales and sand-
stones between. the red beds and the limestone appears to be
500 yards wide, which would give a thickness of 1400 feet if the

_ * While going first through this district I made the mistake of looking on
the uppermost thick bed of coarse sandstone as the top of the Old Red Sand-
stone, and thus assigned too high a position to the base of the Carboniferous
shale group. The sandstones are often very similar in character through a great
thickness, but by disregarding them and looking solely to the characters of the
shales and slates interstratified with them, we hit on anatural boundary. As
long as, in descending from the limestone, these shales or slates preserve their
grey or black colours, marine fossils will often be found both in slates and sand-
stones; on the other hand, as long as, in ascending in the Old Red Sandstone,
the shales or slates show bright-red colours, no marine fossils will be found in
either. The instances of any alternation of red and grey slates are very few, even
if they really exist at all, so that in an ascending section the first black slates, in
a descending one the first red or purple slates, will give the boundary between
the Carboniferous series and the Old Red Sandstone with great approximate
exactness.

334. _ PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

dip were steady for the aisle distance. Possibly 900 feet would
not be far from the real thickness.

Proceeding up the Cork and Midleton trough to the westward,
the next es instructive section will be one drawn north and south
through Carrickshane, near the town of Midleton, to the Old Red
Sandstone hills on the north.

Fig. 6.—Section across Bilberry Hill.

8. Roxborough WN.
House. Bilberry Hill. ae
Biv 4 vr
! xt + = yj \y \) \
reer CASES INE ZANE LANNE
GA aaa 0 Tr Sf EK

Lx Sst
eel y Mi Ws £3
-Htt ikl \\ ! Tree suas KEK
Bee ry ses TNT aan SNe

He y Le YA\Y We \
PRS LESS Sak (Vy XN) \- \\ AN
eA —\ AN
ce
Length of Section, 34 miles,

d?, Thick-bedded grey limestone with fossils.
d. Carboniferous Limestone. { d'. Dark-grey slates with white and brown sand-
stones.
ce. Old Red Sandstone ...... Red slates with red and brown sandstones.

The thickness of the slates here is not exactly determinable, as -
the exposures are few and scattered, and one of them gives a dip of
10° to the north, indicatmg an anticlinal curve. The quarries and
cuttings, however, which were opened at Bilberry Hill in the year
1851, when the late Edward Forbes visited this locality with me,
were crowded with the little cases of Crustacea which were then
called Cypris, since Cypridina, and are now known as Leperditia.
Forbes was greatly struck with these ‘‘ Cypris-slates,” as we then
called them, comparing them with those known on the continent as
Oypridina-schiefer.

The width of the tract at Bilberry Hill, in which grey and blue
slates and brownish and whitish sandstones are interposed between
the massive Carboniferous Limestones and the bright-red slates and
red and green sandstones of the Old Red Sandstone, is about a mile
and a half, but reference to our maps will show that there is a fault
as well as a curve in this tract. A list of the fossils collected in the
Carboniferous Limestone near Midleton, and those found in the grey
slates and grits of Bilberry Hill, drawn up by Mr. Baily, will be
found in the Explanation to sheet 187 of the Irish maps. The
limestone fossils include more than seventy species of Corals, Shells,
&c., such as are most abundant throughout the Carboniferous Lime-
stone of the British Islands. The fossils from the slates are fewer,
and I will therefore quote the list here :—Fenestella antiqua, Orthis
Michelin, Producta Martini, Rhynchonella plewrodon, Spircfera lh-
neata, S. striata, S. Verneuillit (or disjuncta, with the variety called
Mosquensis), Aviculopecten neaikis, Cypricardia Phillips, Modiola
MacAdami, Orthoceras undulatum, Leperditia (Cypridina) subrecta.
' The black slates and dark-grey grits strike steadily along the
south side of the Old Red Sandstone ridge from Bilberry Hill, through
the city of Cork, and on to Cookstown, everywhere dipping south at

1866. | JUKES —OLD RED SANDSTONE AND DEVONIAN. 335

a high angle under the Carboniferous Limestone. They are, however,
often concealed by the alluvial flats which are formed on them by
the river Lee and the branches of Cork Harbour, but may be seen
in many places about Cork; for the details of which I must refer to
the Explanation of sheet 187 of the Irish Survey maps.

7. The Knockadoon and Sheeps Head Anticlinal, and the country to
the south of it, around Queenstown, Kinsale, Bandon, Skibbereen, and
Carrigboy.—The southern margin of the North Cork Old Red Sand-
stone district is formed by a narrow anticlinal ridge of Old Red,
which, as mentioned at p. 330, stretches across Ireland from Knocka-
doon Head to Sheeps Head. Along the south side of this ridge the
dark slates and grits which interpose between the Old Red Sandstone
and Carboniferous Limestone are equally continuous, and may be
followed in the first instance from the north shore of Ballycottin Bay
to Queenstown, and thence by Monkstown, and Myrtle Hill near
Ballea, to Ballinhassig, which is 24 miles west of Ballycottin Bay.
From Ballinhassig, both the Old Red Sandstone ridge and the
dark slates and grits on the south of it, may be followed for still
another 26 miles to Dunmanway, and still farther west, without
any break (except an occasional glen coming through the ridge)
past Dromdaleague to Carrigboy, and down the north side of Dun-
manus Bay, until we come to the lofty vertical cliffs of Sheeps Head
itself.

For the first 20 miles, starting from Knockadoon Head on the east,
the dark slates and grits dip under beds of Carboniferous Limestone
on the south side of the ridge, as they do on the north side of it ;
but the slates and grits on the south side become materially thicker
as we follow them towards the west, until about Five Mile Bridge
and Ballinhassig there is no longer any Carboniferous Limestone
above them. |

Fig. 7.—Section from Ballea across” Myrtle Hill.

8. River N.
Ballea. Owenboy. Myrtle Hill. _ North Fir Hill.
i

. a F
“RU ya - TW .” \V y Wy \
Wim),
dl al.’

\)
\
DAA
ec c
Length of Section, about 3 miles.

d?, Thick-bedded grey crinoidal limestone.
d‘. Dark-grey slates with grey and brown grits.
Baie Pedi Guntletone. .ecck. { runs on green slates, and red and brown sand-

d. Carboniferous Limestone

In fig. 7 we get a diagrammatic section across the valley of the
Owenboy River, a mile or so west of Ballea Castle.” This runs by a
house called Myrtle Hill, and up to one called Fir Hill, which is
about 580 feet above the sea.

Some road-ecuttings, and a little glen which brings a lateral brook
down to the Owenboy, show the rocks well upon the sides of this hill.

336 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 7,

The lowest beds crop out near the hill top, and consist of green and
red slates, apparently horizontal or nearly so; a little farther south
red slates and sandstones dip south at 40° and 50°, greenish flags and
slates are occasionally interstratified with the red slates, and the dip
increases as we go south up to 60° and 70°. Brown sandstones then
come in, with red slates between them at first, but very soon with
grey slates. Bluish or blackish grey slates lie above these, with
occasional bands of brown sandstones and grey grit, the dip being
steady at 50° and 60° to the south. ‘he cleavage in the slates is
also very steady dipping N. 20° W. at 80° or 85°. Grey slates are
seen down to the road, a little south of which, crags of grey crinoidal
limestone appear. This limestone itself is also much cleaved, so that
the bedding is not determinable with any certainty.

Immediately south of this the grey slates rise out again at an angle
of 30°, and are then much contorted, as may be seen in several small
quarries and cuttings, but still better in the little ravine which the
river has cut near Ballea Castle, on its way from this patch of lime-
stone to the western termination of that of Carrigaline. The cleavage
here also dips steadily north-north-west at 80°, through all the
numerous contortions of the beds.

The thickness of the Carboniferous Limestone here cannot be very
great, perhaps 200 feet at a maximum. ‘That of the Carboniferous
slate and grit is apparently about 1500 feet, while the Old Red
Sandstone is exposed to a depth of 4000 or 5000 feet, the lowest
beds being bright-red slates.

The fossils found in the Limestone near Ballea comprise .Amplewus
coralloides, Spirifera pingws, S. striata, Streptorhynchus cremstria,
Actinocrinus variabilis, and other common Carboniferous fossils.
There are several fossil localities in the Carboniferous slate of this
neighbourhood, from one or other of which the following species

have been collected, the specific determinations being made by Mr.
W. H. Baily.

Prants. Filicites lineatus (<‘ linear plants”).

Ca@LENTERATA. Oyathophyllum (Petraia) celtrcum; Pleurodictyum
problematicum*.

Potyzoa. Cerropora rhombifera; Fenestella antiqua.

Bracuiopopa. <Athyris ambigua; Orthis Michelini; Producta sca-
bricula; Rensselleria stringiceps?; Rhynchonella sleurodon ;
Spiifera cuspidata, S.striata,S. Vernewlli (S. disyuncta); Spiri-
ferina cristata, var., octoplicata ; Terebratula hastata.

Concu1FERA. Avicula Damnoniensis; Cucullea Hardingu, (inclad-
ing the varieties amygdulina and trapezium) ; Curtonotus elegans

* This was long familiarly known to us on the Survey under the name of the
“ Belgooly Coral.” Its identification with Plewrodictyum problematicum depends
on Mr. W. H. Baily’s authority. Doubts of the correctness of that identifica-
tion having been expressed by Mr. Salter and others, Mr. Baily has re-investi-
. gated it, and still holds by his opinion that it is either that identical form, or
one very closely allied to it. As it is now believed to be the mere cast of another
coral, minor variations in the form are to be expected. Whatever it be, it is
beyond all doubt identical with specimens from Braunton in North Devonshire.

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 337

_ (and the varieties elongatus and rotundatus); Modiola MacAdam ;
Nucula, sp.; Sanguinolites, sp.
GastERopopA. Acroculia striata; Plewrotomaria, sp.; Turbo, sp.
Hereroropa. Bellerophon subglobatus.
CrpHALopopa. Orthoceras undulatum, and others.
Ecurinopermata. Actinocrinus polydactylus ; Cyathocrinus pinnatus,
and (? Actinocrinus) variabilis ; Platycrinus, sp.
Crustacea. Leperditia (Cypridina) subrecta.

Specimens of Cucullea and Curtonotus were found at several lo-
ealities (see Explanation of Sheet 187, p. 17, of the Irish Survey
Maps), but always in grits, the situation of which showed them to
be low down in the Carboniferous Slate. One very good locality for
those shells is in a small quarry on the south side of the lane leading
westwards to Coolkirky House, near the hill top. The fossils occur
as casts in a band of brown sandstone, about 4 inches thick, which
is almost made up of them, though similar beds both above and
below do not show a single shell. Those sandstones are interstra-
tified with beds of grey slate, all dipping north at 65° (J6., pp. 54, 55).

This occurrence of these Conchifers in vast abundance in some
thin bands, and their total absence through great thicknesses of rock,
is what takes place also in Devonshire, as I saw in the quarries near
Braunton.

Fig. 8.—Section near Ballinhassig.

S. River .g N.
Ballyheedy Owen- 8 Rail-

Chapel. b Goggan’s Hill.

Length of Section, about 3 miles.
d . Probably Coal-measures.
d*, Carboniferous slate with Coomhola grits in lower part.
c. Old Red Sandstone, red slates and grits.

In fig. 8 we have a section on the flanks of the same Old Red
Sandstone ridge as that shown in fig. 7, and across the same valley
of the little* Owenboy river, but a few miles farther west.

The Old Red shows thick red sandstones and purple slates un-
dulating in various directions, but chiefly to north and south, and
finally dipping south at a high angle, the upper beds having much
green slate interstratified with the red.

South of these, strong yellowish-brown sandstones and greenish-
grey and yellow flagstones and shales show themselves in the rail-
way-cutting, and elsewhere, dipping south at 70°, and still farther
south, about the railway tunnel, greenish-grey grits and grey slates
undulating in many regular arches and troughs, but on the whole
dipping south. Interstratified with these sandstones are dark-grey
slates, which increase in number as we pass through the railway-
tunnel to its southern termination, where soft dark-grey shining

* Owenbue, or Yellow River.

338 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

slates, with thin grit bands dip south at 45° or 55°. These are
occasionally very fossiliferous, the species being some of those given
above. Over these are bluish-black smooth lustrous slates with
occasional nodules, about the size of walnuts, or larger, called “ Bulls’
Eyes” by the quarrymen. Down in the road, near the river, they
dip south at 60°. These bluish-black slates become much paler by
exposure to the weather, and might then be described as pale green-
ish-grey chloritic-looking slate, with a soapy feel.

On the south side of the valley, in the lane going up to Ballyheedy
Chapel, we meet first with shining slate similar to that just described ;
but higher up, near the top of the ridge on which the Chapel stands,
the slates become more earthy and blacker, and weather to a rusty
brown. These are more like the shales or slates which occur in the
Trish Coal-measures above the Carboniferous Limestone than ordi-
nary Carboniferous slate; and: having some reason, from the fossils
contained in them, to suspect that they really were Coal-measures, I
visited the district again two years ago, to search for other exposures
in them, but was not successful in finding any, except one little
quarry a mile and a half west-south-west of Ballyheedy at a place
called Rag Bridge.

The shales or slates here dipped at 10° only, to the east, and had
precisely the banded iron-stained appearance, characteristic of the
Lower Coal-measure shales in Ireland. Their surfaces were covered
also with small Poscdonomya*, as is so often the case with the Coal-
measure shales.

The most remarkable evidence for the Gane measure age of these
shales, however, is the presence of certain small skeletons of fish,
found many years ago at Ballyheedy, which, by the advice of the late
Prof. E. Forbes, I submitted to Sir Philip de M. G. Egerton. He
referred them to the genus Celacanthus, a genus which he informed
me he had never known to occur below the Coal-measures. Mr. A.
M‘Henry, one of our fossil-collectors, has found during the past year
some specimens very similar to these, and in precisely the same sort of
black slate, in the Coal-measures of the coast of Kerry near Bally-
bunnion. These latter specimens occurred near the top of the cliff,
a quarter of a mile north of the last exposure of Carboniferous Lime-
stone, in beds which lie about 800 or 900 feet above the top of that
Limestone. 2 ;

Professor Huxley has examined both sets of specimens, and will
shortly figure and describe them; he refers them to his restricted
genus Celacanthus, which he also does not know as occurring below
the Coal-measures.

I believe, therefore, that I am fully justified in referring these
black slates of Ballyheedy to the true Coal-measures, and that we
have in the section, of which fig. 9 is a sketch, the whole series from the
bottom part of the Coal-measures, deep into the Old Red Sandstone,
all conformably deposited. Comparing it with the section at Ballea,
(fig. 7) 5 miles farther east, I believe the Carboniferous Limestone

* They would well deserve the name of Posidonomya-schist, the name given
to beds which I believe'to be the same beds in the Rhine country.

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 339

there to be merely the topmost beds of that formation, and that if
the denudation had spared the rocks a little more, they would still be
covered by the Coal-measures. Coming to the west, that limestone
is evidently becoming debased and dying away, for in the farthest
quarry to the west, while there is one good mass of Crinoidal Lime-
stone, the chief part of it is gritty and earthy-looking, and so impure
that they have ceased to quarry it for burning into lime. Black shales
lie in the ground half a mile farther west, in the lane leading from Old
Five Mile Bridge, and on the hill to the north of it, where impres-
sions of Posidonomya are abundant.

If those black shales, and those of Ballyheedy, are really Coal-
measures, it will show another analogy with Devon, where the Culm-
measures (which are exactly like the Irish Coal-measures) rest on
the Carboniferous slate without the possibility of drawing any decided
line between the two*.

The most obvious conclusion, on comparing the sections of Water-
ford and Kilkenny with those of Midleton, Ballea, and Ballinhassig
(figs. 2 to 8), is doubtless that the Lower Limestone shale has ex-
panded to the south-west, independently of any change in the Car-
boniferous Limestone, and that the beds which form the base of the
Limestone at Ballea are the same beds which are the base of the
Limestone at Waterford, for instance: This, however, is not a ne-
cessary conclusion, and I now believe that the limestones die away
from below upwards in proportion as the shales or slates be-
come thicker; so that what appear to be the lowest beds of Car-

boniferous Limestone in the south-west, are on the same geological
_ horizon as the upper beds of the limestone to the east and north.

Owing to the want of continuous sections, and the frequent un-
dulations of the beds, it is impossible to assign very accurate thick-
nesses to the several rock-groups in the Ballinhassig section, fig. 8.
Perhaps we might calculate the Ballyheedy Coal-measures at 500 or
600 feet thick ; the thickness of exposed Old Red Sandstone as 1500
feet; and the Carboniferous Slate, between the two, as showing a
thickness, which may be as little as 3000 feet, but may be as much
as 5000 feet, or more.

8. Old Head of Kinsale.—The greater estimate is certainly not
too great for the thickness of the Carboniferous slate a little farther
south, about Kinsale for instance. The narrow promontory which
is known as the Old Head of Kinsale stretches out to the south for
3 miles, with vertical cliffs on each side of it. The beds strike east
and west from one cliff to the other, and can be examined on both
sides from a boat, and are occasionally accessible on land. Their
general dip is north, at angles varying from 40° to 80° or 90°.

_* Mr. Godwin-Austen describes the limestone of Ugbrook Park, near Newton
Bushel, in South Devon, as Carboniferous Limestone with Devonian (or Strin-
gocephalus Limestone) below it. Although I have not yet been able to visit the
locality, I have no doubt of its being accurately described by Mr. Godwin-Austen,
and that the Ugbrook Park Limestone is like that of Ballea, just the uppermost
beds of the true Carboniferous Limestone, with the Carboniferous Slate lying
under it, enclosing inliers of Stringocephalus Limestone, and some of the peculiar
forms of fossils to which the name “Devonian” has been assigned.

340 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

At the extreme southern point of the head they consist of hard
greenish-grey grits, which we at first took for the upper part of the
Old Red Sandstone, but which are the same as those afterwards
called the Coomhola grits.

These undulate in very regular troughs and saddles, dipping north
and south respectively at angles of 40° or 50°. Over them comes a
great series of grey slates and grey and greenish grits, the dip being
steady to the north at 60°, for a distance of a mile and a half. The
beds then become more purely argillaceous, black shining slates, with
occasional bands of nodules, and grey slate weathering to a light-
green tint with a soapy feel. The cleavage is often vertical, but in
Holeopen Bay was noted by Mr. Du Noyer as dipping to south-south-
east at 60°, and again in another place to north-north-west, at 80°. To
the northward of Ringalusky point and Black Head, undulations occur
again in beds of grey slate, but still with a general dip to the north,
until we reach Ballymackean on the east coast, and Lispatrick Lower
on the west, where the promontory unites with the main outline of the
coast. The slates here are black, and carbonaceous, and on the
Lispatrick side there occur numerous specimens of Posidonomya
Becheri, Goniatites, and small Orthoceratites, making it probable that
we here again have some of the basal shales of the Coal-measures
brought in on the top of the Carboniferous Slate. Immediately to
the north of this the beds rise again to the north for a long way, as
may be seen by following the cliffs, eastwards towards Kinsale Har-
bour, or westwards along the shores of Courtmacsherry Bay.

Mr. Du Noyer, after making all allowance for the undulations of

the beds, calculated that the thickness exposed in the cliffs of the
Old Head promontory cannot be less than 6500 feet (see Explanation
of sheet 194, &e. p. 23).
_ 9. Cape Clear and Mizen Head Anticlinals.—Between Ballinhassig
and the Old Head of Kinsale, a distance of 15 miles from north to
south, no.Old Red Sandstone reaches the surface from underneath the
Carboniferous slate, notwithstanding the numerous anticlinal and
synclinal curves which run through the country. Proceeding towards
the west, however, two main anticlinal ridges of Old Red rise
gradually from underneath the Carboniferous ‘slate, increasing in
width and importance as we proceed further west, and terminating,
the southern one in Cape Clear Island, and the other in the Mizen
Head. Minor undulations also bring up the Red Rocks on both
sides of Clonakilty Bay, forming the headlands called the Seven
Heads and Galley Head, and also in Roaring Water Bay, continually
sub-dividing and narrowing the area of Carboniferous Slate.

The Old Red of the Mizen Head anticlinal makes its first appear-
ance in the hill of Knockawadra, 5 miles south of Dunmanway%*,
stretching thence to the Mizen Head. It was on the south side of

* Tn our published maps, this anticlinal is marked as showing Old Red Sand-
stone several miles farther to the eastward; but I now believe that the strong
green grits and slates which were at first supposed to indicate the top of the Old
Red Sandstone, belong in reality to the Coomhola grits in the Carboniferous
Slate. :

1866.]

Fig. 9.—Section from Reenydonegan Lough across Coomhola Mountain to Priest’s Leap.

Reenydonegan

my

\

WS
SN

W
SN

NN)

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LISTS SES
XX

Length of Section, about 7 miles.

(Coomhola grits) in the lower part. ;
Alternations of purple and green clay-slates, and purple and green grits; some of a peculiar type, called

Black glossy slates with (XX) calcareous bands in the upper part, and hard siliceous greenish-grey grits

S|

d. Carboniferous Slate ...

JUKES—-OLD RED SANDSTONE AND DEVONIAN.

c. Old Red Sandstone ......

“ Glengariff Grits.”

341

this anticlinal, 2 miles north-
west of the town of Skibbe-
reen, in a lane running by the
R. C. Chapel of Abbeystrowry,
in the townland of Mohanagh
(just under the name Clashee-
nagnaw, as engraved on the
one-inch map), that Mr. Salter
and the late James Flanagan
and I met with the large casts
of Cucullea, and other fossils
mentioned in a paper by Mr.
Salter and myself, published
in the ‘Journal of the Dublin
Geological Society,’ vol. vii.,—
‘¢ rounded, sharply keeled, and

‘trilobated species of Bellero-

phon” were found here, as well
as a large Lingula, the large
Cucullea, called afterwards by
Mr. Salter Cucullea Griffithu,
abundance of Avicula Damno-
neensis and Rhynchonella pleu-
rodon, and other shells.

10. The Bantry Bay Trough.
—On the northern side of the
Mizen Head anticlinal lies the
trough of Carboniferous Slate,

’ the western extension of which

runs down Dunmanus Bay.
On the northern side of that
trough we again come back to
the ridge of Old Red mentioned
before as stretching from
Knockadoon Head to Sheeps
Head, and forming the south-
ern margin of the North Cork
Old Red Sandstone district.
The exposure of Old Red Sand-
stone in this ridge is very nar-
row just south of the town of
Bantry, the beds being nearly
vertical, with almost vertical
beds of Carboniferous Slate
(containing Coomhola Grits) on
each side of it. The inter-
vening space of red slates and
grits is barely a mile wide in
one part. |

To the northward of this lies

342 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

the Bantry Bay trough of Carboniferous Slate, which is five miles in
width. The beds are admirably exposed in the cliffs on both sides
of the Bay and in the various hill-sides and brook-channels, as far
into the country as the eastern base of Shehy Mountain (See Ex-
planation of Sheets 192, &c., of 193, of 197, &., and of 198; also
Sections, sheets 19, &c.). Fig. 9 is a section on the north side of
this trough in the neighbourhood of Coomhola. |

The beds may be thoroughly examined here, either on the sides
of the Coomhola River above Snave Bridge, or on the shores of the
Bay from Reenagough Point into Glengariff Harbour. Fossils may
be got from the shores about Reenagough and Ardaturrish Points
pretty plentifully, but only with much labour and breaking-up of
the rocks by strong and heavy hammers.

The dip here is steady to the south by east at 75° or 80° for a
mile and a half at least, with scarcely an interval in which rock is
not observable.

If we take the distance across the edges of the beds at 8000 feet,
and allow a dip of 75°, this gives us a thickness of 7760 feet. Of
this thickness we may assign 4000 feet to the Old Red Sandstone,
taking the uppermost bed of purple slate as its upper boundary.
This boundary may be seen at a little cove on the northern part of
Ardaturrish townland, where the shore bends to the westward in one
direction, and southwards in the other. South of that there are no
red rocks, the grits being all greenish-grey, and interstratified with
dark-grey or black slates. The beds of grit are 2 or 3 feet thick,
and they occur in groups 200 or 300 feet in thickness, with bands
of grey slate of similar thickness between them. They strike steadily
from this shore through the Coomhola Glen and along the hill-sides
for ten miles to the eastward, and are frequently and largely exposed
through the whole distance. They must have an aggregate thick-
ness of at least 3000 feet. Above them is a great thickness of black
shining slate, probably 2000 or 3000 feet more, in the upper part of
which are calcareous bands, becoming in some places crystalline
limestone in beds of 2 feet in thickness.

Mr. Salter and I, with James Flanagan, collected the following
fossils when examining the Ardaturrish shore several years ago :—
LInnear Plants, both in the uppermost red rocks and the lowest
grey beds; and a stem of the plant called Anorria (? Sagenaria) in
the grey grits*; Avicula Damnonensis, Cucullea trapezium, Cur-
tonotus elegans; species of Lingula, Modiola, Pileopsis, Cythere
(Leperditia), besides Rhynchonella pleurodon and other Carboniferous
Brachiopoda. In the more purely argillaceous parts of the Carbo-
niferous slate, and especially in the calcareous portions of it, Encri-
nites and Brachiopods abound, the principal of the latter belonging,

* In the fine work lately published by the Société des Sciences Naturelles,
of Strasburg, entitled ‘Le Terrain de Transition des Vosges,’ by J. Keechlin-
Schlumberger and Prof. W. Ph. Schimper, the latter learned gentleman has
described and figured several fine specimens of these plants, which seem to be
precisely identical with those which are so abundant in the upper part of the
Old Red and the lower part of the Carboniferous Slate of Ireland.

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN, 343

according to Mr. Baily’s determinations and Mr. Davidson’s confir-
mation of them, to Athyris Royssw or A. concentrica, Chonetes Hard-
rensis, Cyrtina heterochita?, Producta scabricula, P. semireticulata,
Rhynchonella pleurodon, Streptorhynchus crenstria, Spirifera lami-
nosa, N. striata S. Vernewilla (disjuncta), and Spiriferina cristata,
var. octoplicata. :

These are especially numerous at Reenydonegan point, which is
made of about the highest beds of the district, where Phaillipsia
pustulata was to be got in great abundance, and where, in addition
to the above-enumerated species, the following were also procured:—

Alveolites depressa, Cheetetes tumidus, Cyathophyllum (Petraia)
celticum, Fenestella antiqua, Glauconome pluma, Polypora laxa,
Pullastra bistriata, Acroculia vetusta, Bellerophon subglobatus, and
Cyathocrinus variabilis.

Although the highest in the district now, and 5000 or 6000 feet,
at least, above the top of the Old Red Sandstone, it must be recol-
lected that we have no proof of these being originally the highest
beds of the Carboniferous slate.

11. The Berehaven Promontory and that of Iveragh and Dunkerron.
—We can penetrate in many directions to a depth of many thousand
feet into the Old Red Sandstone by means of the numerous glens and
ravines in the Glengariff country and throughout the mountainous
ground between the valleys of Bantry and Kenmare, or in that between
Kenmare and Dingle Bay. In some of these deep recesses, which cut
directly across highly inclined beds dipping steadily in one direction for
a mile or two at atime, we must come down to beds which are 8000
or 10,000 feet below the base of the Carboniferous Slate. In no one
instance, however, either there or elsewhere throughout Ireland, did
we find any dark-grey slate or any marine organic remains in or
below the Old Red Sandstone, until we.came down to Silurian rocks
and fossils. The prevailing colours of the rocks are red of different
tints, alternating with different shades of green. Massive sets of’
grits (of a kind called by us Glengariff Grits) and thick bands of
slate occur of both these hues; but no change, either lithological,
paleontological, or stratigraphical, which would enable us to draw a
lower boundary to the Old Red Sandstone, and say that we had got
into any other formation lying below it, is to be found south of
Dingle Bay.

Sir R. I. Griffith does indeed draw a boundary in the middle of
these red rocks, and considers their upper part only to be Old Red
Sandstone, and the lower to be Uppermost Silurian. I believe,
however, that this has been done in order to make the divisions south
of Dingle Bay analogous to those in the promontory immediately to
the north of it. We were unable to discover any characters which
would enable us independently to make such a subdivision to the
south of that Bay. That the upper portion, at least, of this great
mass is really Old Red Sandstone is beyond a doubt, since it is
physically continuous with those masses in the eastern part of Cork,
and in the counties of Waterford and Wexford, to which no English
geologist could refuse that name.

344. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

12. Dingle Beds.—Although it has no direct bearing on the subject
of this paper, it may still be pointed out that in the promontory north
of Dingle Bay, the Old Red Sandstone differs somewhat from that
just described, both in lithological character and in the thickness and
lie of the beds.

In the Dingle Promontory the Old Red Sandstone contains much
more conglomerate than it does south of Dingle Bay. It has large
masses of quartzose conglomerate, and also a very singular local mass
containing chiefly angular fragments of granite, gneiss, mica-schist,
felstone, and gritstone. This is sometimes as much as 400 feet thick,
but thins out rapidly in each direction. We have spoken of it as
the “ Inch Conglomerate ” (see Mr. Du Noyevr’s descriptions in Ex-
planation of Sheet 160, &c., pp. 6, 14, and 41).

This Old Red Sandstone rises conformably from under the base of
the Carboniferous Limestone and has a thickness of 3,000 or 4,000
feet, but it rests quite unconformably on some highly inclined red
rocks,—slates, sandstones, and conglomerates,—which have a much
greater thickness and a rather different lithological character. These
seem to repose conformably on Ludlow and Wenlock rocks at Dun-
quin and Ferriter’s Cove. We have provisionally designated them
as the Dinetze Brps. They are at least 10,000 feet thick. Their
conglomerates differ both from the Inch and the quartzose conglom-
erates of the Old Red Sandstone, their pebbles being chiefly rounded
and angular pieces of brown sandstone, in some of which Llandovery
fossils were found. ‘The Dingle beds also contain beds of blood-red
slates of a brighter colour than any usual in the Old Red Sandstone
of Cork or Kerry. On the other hand, their sandstones and grit-
stones are very much the same as those found in the rocks of the
Iveragh and Dunkerron Promontory, south of Dingle Bay, especially
some peculiar-looking sandstones lithologically identical with the
“ Glengariff Grits.”

While, then, I cannot by any means feel sure that some of the
lowest rocks seen in the country south of Dingle Bay are not the
DINGLE BEDS, it was thought best not to assert that as a fact
without further proof, and each district has therefore been coloured
in our maps according to its own evidence. In the Dingle Promon-
tory the beds on which the Old Red Sandstone rests unconformably
are separated from it as “‘ Dingle Beds.” In the maps of the other
district the colour used to distinguish the uppermost beds, which are
undoubtedly Old Red Sandstone, is continued over the lower ones
because we failed to discover any characters which would enable us
to draw a lower boundary to them.

_ 18. Gradual Changes in Inthological Character—It must not
be forgotten that in thus tracing these continuous masses of rock
across such large portions of Ireland there occur gradual lithological
changes in them, which might easily mislead an observer who saw
them only at distant intervals. Any one who visited only the Old
Red Sandstone of Waterford, and then went at once to Glengariff in
Bantry Bay, without examining the intermediate district, might de-
cline to believe that the Old Red Sandstone there was part of the

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 345

same formation as that of Waterford. In like manner any one who
studied only the Carboniferous Slate about Cork Harbour, or even
about Kinsale, might look upon the Coomhola Grit portion of that
group in Bantry Bay, and in the western Headlands of Cork, as
something wholly different.

I can speak from personal experience on this point, as I myself
made mistakes when first mapping the rocks of Bantry Bay, trusting
to the ideas gained about Cork Harbour. The identity of the rather
dissimilar rocks in different parts of the country came out as the
final result only of the Survey, when the beds had been patiently laid
down on the six-inch maps (in the course of several years’ labour),
entering on those maps merely the data shown in each locality as it
was passed through. The monotony of this task can scarcely be
understood by amateur geologists, who are at liberty to select
their localities and pick out the more interesting and important bits.
Its value, however, becomes understood on its completion, when the
results are gathered from a mass of data collected by different ob-
servers working independently without any foregone conclusions to
vitiate their observations. :

14. General Conclusions on the Rocks of the South-west of Ireland.—
One general conclusion may be briefly stated as the result of the ex-
amination of the western part of the county Cork, namely, that there
are two great formations in it, the Old Red Sandstone below, and the
Carboniferous Slate above; the Old Red Sandstone containing no
marine fossils and scarcely any fossils at all, except plants in its
upper portion; the Carboniferous Slate containing some of these
plants, but also marine fossils, sometimes in great profusion. The
Old Red Sandstone has a prevailing red tinge throughout, with no
beds of black or bluish-grey slate; the Carboniferous Slate has a
prevailing black or bluish-grey colour, with no beds of a red tinge.
Both are greatly affected by slaty cleavage.

It may also be stated that where the Carboniferous Slate and Car-
boniferous Limestone are both present together, the Carboniferous
Limestone is uppermost; but that where the Carboniferous Limestone
has a thickness of 2000 feet, or upwards, the dark slates between it
and the Old Red Sandstone are very thin, rarely more than 200 feet
in thickness ; while where these dark slates thicken out to more than
2000 feet, there is no great thickness of Carboniferous Limestone over
them. Where the Carboniferous Slate attains a still greater thick-
ness, and swells out to three, four, or five thousand feet, it has never
any Carboniferous Limestone over it at all, but there appear here
and there patches of black slate upon it, which both lithologically
and paleontologically resemble the Coal-measures. If so, the Car-
boniferous Slate occupies, there, the whole interval between the top
of the Old Red Sandstone and the base of the Coal-measures, with a
perfectly conformable and continuous series of beds to the exclusion
of the Carboniferous Limestone; and therefore replaces that
Limestone. Dark grey mud and sand were at first deposited over
the whole area, but were subsequently restricted to a part of it,
where they continued to be deposited in great quantity; while in the

VOL. XXII.—PART I. 2B

346 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

rest of the area clear water prevailed, in which limestone was formed
from the Crinoids and other animals that flourished in that part.

15. Sudden Changes from thick Limestone to Mechanically formed
Rocks.—Many persons may feel a difficulty in supposing it possible
that a sudden change can take place from thick limestones to mere
slates and sandstones. My own experience among coral-reefs, how-
ever, relieves me from any such difficulty. The barrier-reefs of the
north-east coast of Australia, for instance, are continuous for about
1200 statute miles, and have a steep edge throughout that course,
which in one part at least is upwards of 1800 feet in depth. They end
against the coast of New Guinea, on the north side of Torres Straits,
in a massive reef, called the Warrior Reef, which is itself thirty miles
long and as massive, and steep too, though by no means so deep, as
any other reef to the southward. Immediately east of it, however,
the coast of New Guinea is fronted by extensive mud-flats; and
shoal water, with a muddy and sandy bottom, stretches off the coast
for sixty miles from the shore; and the land consists of mangrove-
swamps for an unknown distance into the interior, and this for a
space of 150 or 200 miles along the coast. There must then be as
abrupt a change here as we can imagine, from a widely spread and
continuous calcareous mass, to one consisting principally or entirely
of a mechanically formed deposit.

No one can study the Carboniferous Limestone minutely without
seeing that it is essentially composed of crinoidal fragments. Even
in the compact parts of the limestone, examination with the lens will
disclose many little shining faces of crystalline Calcite with a dot in
the middle, which Professor John Phillips long ago pointed out to
me as a sure indication of a crinoidal joint. The limestone has been
formed by the growth of submarine forests of Encrinites; the debris
of each successive generation being ground down or decomposed into
calcareous mud. So far as the circumstances of depth and bottom
favoured the growth of these animals, they flourished; where there
occurred a sudden change in those circumstances, they ceased to grow.
The very incoming of quantities of mud and sand would be one of
the circumstances most likely to arrest their growth. The animals
inhabiting seas with a sandy or muddy bottom would naturally be
somewhat different from those living in the clear water among the
forests of Crinoids. Neither would it appear to me at all surprising
if, when circumstances favourable to the growth and formation of
local banks of limestone occurred within the muddy and sandy area,
some animals should live there of a different species or genus from
those in the other part of the sea where the crinoidal forests grew.

III. Grorogicat Structure or Norra Devon.

1. Baggy Point to Dulverton.—In a paper read before the Dublin
Geological Society * on May 10th, 1865, and published in their

‘* The name of this Society has lately been altered by Her Majesty’s per-
mission into that of the Royal Geological Society of Ireland, the members being
empowered to call themselves Fellows thereof.

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 347

Journal, I went at length into the reasons which induced me to

identify the beds about Barnstaple, Pilton, Marwood, Braunton, and

Baggy Point with the Carboniferous Slate of Cork, and the red beds

- Vention in Morte Bay with the top of the Old Red Sandstone of
ork.

The greenish and brownish grits, containing large Oucullew, &c.,
known as “‘ Marwood Sandstone,” are represented in Ireland by
similar sandstones with the same fossils as mentioned at pp. 336, 337.
These sandstones expand in Bantry Bay into the great mass which
there acquired the name of “‘ Coomhola Grits.” I believe, however,
that any attempt to separate these beds, either in Devon or Ireland,
as a distinct group from the Carboniferous Slate in which they lie,
will merely mislead us. Both the sandstones, and the peculiar fossils
which they contain, are local occurrences, either, or both of which
may be present in, or absent from, the same formation in different
districts. I satisfied myself during the excursion in 1861, of which
the paper mentioned above gives an account, that the Old Red Sand-
stone which crops up in the south corner of Morte Bay, is continuous
into the country at least as far as the moor called Span Head on the
Ordnance Map*, a distance of about twenty miles; and that the
Carboniferous Slate continues that far to the south of it. The time
at my disposal did not allow me, on that occasion, to do more than
take one walk from Barnstaple across to Ilfracombe and back, and
what I saw during that traverse merely bewildered me. There
was apparently a prevailing dip to the south all across the country,
nevertheless the rocks about Ilfracombe were very unlike any that I
knew of in the Old Red Sandstone of Ireland, and had a certain resem-
blance to parts of the Carboniferous Slate. Not finding any fossils,
however, I hesitated to do more than hint at a doubt whether “ the
Ilfracombe beds were really below the red beds of Morte Bay,” and
to suggest a suspicion that they “may belong to the Carboniferous
Slate rolled in to the north by contortions, and somewhat different
lithologically from those farther south” (loc. cit. pp. 10 & 11).

After the meeting of the British Association in Birmingham last
year, I hoped I had secured an opportunity of satisfying myself on
this point. I had carefully re-read and made an abstract of the paper
by Professor Sedgwick and Sir R. I. Murchison in the fifth volume
of this Society’s Transactions, and had in consequence dismissed from
my mind the suspicion mentioned above, and set out with the full con-
viction that the rocks of the north coast, about Lynton and Ilfracombe,
could not be in any way the same as those near Barnstaple, and was
accordingly prepared to find a series of rocks wholly new to me.

- 2. Dulverton.—I made first for Dulverton, some ten miles farther
east than any ground I had yet seen. I found, as I expected from
the published descriptions fT, that the Carboniferous Slate and Old

* The people of the country give the name of Span Head to another hill two
or three miles farther to the east.

Tt See especially the fossils mentioned by Phillips as occurring at Bmationd:
near Dulverton, in his ‘ Palxozoic Fossils.’ I collected Orthis interlineata in a
quarry there.

232

— «348 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 7,

Red Sandstone of the Barnstaple district continued steady in their
strike to the eastwards to at least some miles east of Dulverton.
The Carboniferous Slate, however, appeared to me to be getting
thinner to the eastward, apparently by reason of the dying away of
the sandstones contained in it. That the Marwood Sandstones were
still represented was evident from the abundance of subangular
blocks and angular fragments of their peculiar kind of stone, in the
lanes and ditches and fields along the strike of the lower part of the
Carboniferous Slate; but they did not appear to be quarried, neither
did I succeed in finding any fragments containing fossils. In the
lanes near a place called Crewsball* in the Ordnance map, a mile
west of Dulverton, the rocks shown in the ditches were exactly like
those in similar ditches near Marwood. A mile to the east of Dul-
verton, too, by the lane-side going over the hill to Burry, there is
one little disused quarry in which these sandstones can be partially
observed, and they appeared to be perpendicular, striking E. 10°
north. The cleavage in all the slate beds about Dulverton strikes
about east-north-east and west-south-west, dipping either north or
south at high angles. The beds also dip occasionally to the northward,
showing that they are either undulated or inverted in places.

8.

_ Fig. 10.—Section East of Dulverton.
hi)

£ N.
Upcot. Gulham. Dulverton Common. River Barle.

|
L |
dl al

SS

——
=
iS

—

——|
—S>-

SS

—S—~
—

ee 7 a
art SIAR Ae)
a ie ne

Length of section about three miles.

SS

d*, Coal-measures.
d. Carboniferous ...... ad‘. Carboniferous Slate with Marwood Sandstone in
lower part.
Red, yellow, and greenish sandstones interstratified
e, Old Red Sandstone. { with greenish and reddish slates.

The sections most interesting to me, however, near: Dulverton,
were those in the Old Red Sandstone, on the sides of the valleys of
the rivers Barle and Exe. Just north of Dulverton, in the valley
of the Barle, there are large quarries in rocks precisely identical
with those seen in so many places in the south-west of Ireland at
the top of the Old Red Sandstone. Hard, massive, fine-grained grits
of various tints of yellowish white, pinkish red, greenish yellow, and
dark-red, and purple, interstratified with bands of green and purple
clay-slate, dip south or south-south-east at angles varying from 40°
to 70°, with occasional short rolls to the northward. The cleavage
sometimes imparts a sort of grain even to the sandstones, at right
angles to the bedding. In one mass of bright-red slate, where the

* No such name as “ Crewsball’”’ was known to the people, the place being

called ‘‘Willway.” In like manner ‘Old Hollom,” a neighbouring farm, ought
to be “Old Burry.”

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 349

beds were perpendicular, the cleavage certainly dipped north-north-
west at 65°.

Higher up the valley of the Barle, the rocks and the scenery were
precisely those of many valleys about Glengariff and Killarney. In
the lane going up from Ashwick Bridge (a. mere foot-bridge called.
‘‘a clammer” over the Barle) to Dulverton common and: there-
abouts, there were many small exposures of rock, of which the fol-
lowing notes occur in my note-book :—“ purple sandy slate with
grit-bands, strike east-north-east, perpendicular, genuine Old Red
Sandstone of Ireland.” <“Cleaved red sandstone, or sandy slate, pre-
cisely like Old Red Sandstone of Ireland, dip south-south-east at 40°.”

Fig. 10 will give a general idea of the facts to be observed near
Dulverton. |

3. Dulverton to Dunster.—Having thus satisfied myself that the Old
Red Sandstone below, and the Carboniferous Slate above, were con-
tinued thus far to the east without any material change in their
characters from those that they possess in the Barnstaple country, I
proceeded to explore the country to the north, and took the road to
Dunster. I was disappointed in the sections on the sides of the Exe,
north of Chilly Bridge. There are only occasional small road-cuttings,
showing pale greenish-grey soapy slate, in which I was unable to
determine the bedding with anything like certainty.

These rocks are evidently the “ Green * Chlorite Schist with quartz
veins” of Sedgwick and Murchison, appearing to dip under the
“schists and thick sandstones, red and variegated,’ which are as
obviously the rocks which I have just spoken of as Old Red Sand-
stone. The two kinds of rock were nowhere exposed in any close
proximity to each other. |

Respecting some cuttings a little 8. of Exton, I find in my note-
book a remark to the effect that ‘‘it is not easy to distinguish these
from some parts of the Carboniferous Slate ;” though when I wrote
_ that, I was under the thorough conviction that I was deep in the Old
Red Sandstone, or in some still lower formation. The cleavage here-
abouts dipped to the south at 40°, and the beds at first sight seemed to
coincide with it; though patient hammering disclosed in some places
what appeared to be the lamination of deposit dipping northwards.
At Eyeson Hill, between Exton and Wheddon’s Cross, an iron-mine
was opened on a green hill-side, from which a considerable quantity
of hematite had been extracted. Reaching Wheddon’s Cross, which
stands on the crest of the watershed between the basin of the Exe
and that of the Dunster brooks (and appeared by my aneroid
barometer to be about 830 feet above the sea), | went to examine
some old lime-quarries there. In these there were beds of grey
slate, becoming in some places very calcareous, and also inclosing

* The green colour in sandstones and slates was formerly attributed to the
presence of chlorite, without hesitation. It is probably quite as often due to the
presence of the silicate of protoxide of iron. With respect to these slates I
believe that the green colour only appears on the weathered surfaces, and that
when quarried they yield dark-grey or black slates. In each case they have ofter
a peculiar lustrous surface and soapy feel.

350 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

some beds, six or eight feet thick, of pale-grey crystalline limestone.
Both beds and cleavage dipped south at 60°. I did not see any fossils,
except nests of what I concluded was Favosites polymorpha occurring
in branching clusters, somewhat as Fenestella does sometimes in the
Carboniferous Limestone. It is probably to the growth of this coral
that the limestone is due.

These calcareous bands are described by Sedgwick and Murchison
as stretching from Combe-Martin to this place, and then sweeping
round Croydon Hill.

4, Dunster to Lynton.—On the road from Dunster to Lynton, there
were no good exposures of-rock ; though a detailed search in the beds
of the brooks and the cliffs of the sea-shore would doubtless disclose
sufficient to enable a hard-working geologist to make out the struc-
ture of the country. Speaking generally for Exmoor and the neigh-
bourhood, the absence of any good continuous sections is remarkable.
High, wide, gently undulating moorlands, covered with short heather,
or lower cultivated ground with the same gently undulating surface,
are the prevailing features of the country. It is only where the
brooks cut deep into the ground on their way to the sea, or where
the sea itself has cut back into the land and formed cliffs, that any
rock is seen, except in a few small, widely scattered quarries and
little road-cuttings.

The rocks thus shown on Porlock Hill seemed to me not unlike
parts of the Irish Old Red Sandstone.

5. Lynton* and its neighbourhood.—My very first walk, however,
after arriving at Lynton, through the Valley of Rocks and along the
footpath over the cliffs, showed me, to my no small astonishment,
that I was again among rocks belonging to the Carboniferous Slate.

The picturesque crags, so well known to tourists, and the cliffs,
from the pebble beach on the shore to the top of the hill south of
the Valley of Rocks, all showed beds which were as familiar to me
as Chalk is to an inhabitant of Dover, or Oolite to the dweller in
Bath or Cheltenham. The blue-grey slate with little lighter-coloured
bands of grit, giving a stripe to the slates, the beds of hard grit
often highly calcareous, and crowded with fragments of crinoids, and
others more purely siliceous and destitute of organic remains, were
all precisely identical with those which stretch for so many miles
along the shores of the bays of the deeply indented coast of Cork, or
sweep into the interior of that country round so many anticlinal
ridges of Old Red Sandstone. The numerous fragments of Brachio-
poda and all the other fossils seemed to my eyes also to be the same
as those of Ireland. The colour and aspects of the weathered rocks |
were also exactly similar.

As the hill-tops south of the Valley of Rocks appeared from my
pocket aneroid to rise to a height of 1300 feet above the sea, and the
rocks dipped south at 10° or 15°, there could hardly be a less thick-
ness seen in them than 1500 feet, and they are so well exposed that
almost every bed might be seen somewhere or other (see fig. 11).

* In almost all geological works this name is spelt Linton. In the place itself,
however, it is always written Lynton, and the river is called the Lyne.

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN, 351

Fig. 11.—Section across the Valley of Rocks.

Red-stained Valley Barbrick Mill on
bands. of rocks. Road. the W. Lyne.

' I

!

' t

t {
1

i {

; I

wos WSK
ANU WN ES :
AX AS

SAS
WANE SS

Of. en oe on we ae es

Length of section about 14 mile.

Dark bluish-grey slate with calcareous and quartzose grit bands, the lower or
Coomhola-grit part of the Carboniferous Slate.

Along the coast, and in parts of the interior, the grey rocks are stained exter-
nally of a bright red in parallel bands.

Subsequent explorations along the coast by Woodabay to Heddons
Mouth and round by Parracombe, up the glens of the East and West
Lyne, and across the country to Simonsbath, only confirmed me in
the conviction that the whole, or nearly the whole, of the district
consisted of Carboniferous Slate. Whether the upper part of the
Old Red Sandstone rises from beneath it in a narrow anticlinal curve,
or even more than one, anywhere between the coast and the water-
shed of the Exmoor ridge *, or whether the brown sandstones and
thick green grits which I saw in the bed of the brook near Spar-
hanger, and in a little quarry on Farley Down, were in the Car-
boniferous Slate (a part of the Coomhola Grit), I could not exactly
decide.

There was also a band of rock at Lynton, in the Carboniferous
Slate, rather different from any I know in Ireland. This is a
mass of greenish, close-grained, siliceous grit, with liver-coloured
blotches, which is perhaps 200 feet thick, and from its hardness
often makes a conspicuous feature. It is shown in the cuttings of
the upper part of the road from Lynemouth to Lynton, and the
Castle Hotel at the latter place stands on it. In some places there
are small beds or still smaller patches of grey clay-slate in it. In
the road-cutting it sometimes assumed the appearance of a bright-
red grit, but diligent hammering showed that this red colour was an
external stain derived from the peroxidation of some ferruginous
vein-stuff, which had filtered into all the joints and crevices of the
rock. All along the cliffs, from Lynton to Heddons Mouth, the grey
rocks are similarly stained by one or two parallel bands of bright-

* Just as I was sending in this paper to the Society, I received the February
number of the Journal (No. 85), and in the paper by Mr. Godwin-Austen on the
submerged forest of Porlock, I perceive the rocks about Porlock, and thence to
the valley of the Hast Lyne, described as “hard, splintery sandstones, grits, and
pebble beds, with partings of compact shale, the whole series being of various
shades of red,” and “very distinct from the grey slaty rocks with calcareous
bands” and marine fossils which extend southwards from Lynton. This con-
firms the suspicion I had formed that the Old Red Sandstone, which must lie at
no very great depth under the Lynton rocks, rises to the surface towards the
east, perhaps in one low anticlinal, perhaps in more than one, the axes of which
strike nearly east and west, with a slight rise towards the east.

302 _ PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

red ferruginous matter, 20 or 30 feet in width, striking steadily
with the strike of the rocks, but dipping south at much higher
angles. ‘The rocks dip south at angles gradually increasing from 5°
to 30°, but the red ferruginous bands are inclined at angles of 50°
or 60°. The rock thus stained red externally, is dark grey when
first broken open, but the red ochre is in such quantities, and so
readily stains the hammer and the fingers, that even a fresh fracture
is apt to get raddled soon after it is broken, if precautions are not
taken to prevent it.

These red ferruginous bands are very deceptive when viewed from
a little distance, and especially when seen from a boat, as they look
precisely like beds of red rock, and have, I believe, been taken for
such beds by some previous observers.

I believe I detected the origin of the ochre, at the cove of Heddons
Mouth, in little plates and strings of hematite in the quartz veins
there. These quartz veins traversed certain beds of rock in great
quantity without penetrating beyond them, either above or below ;
and the hemitite occurring as nests in their cavities would when
weathered be naturally converted into red ochre.

T also observed at Heddons Mouth a mass of grey grit, curiously
marked on the surface with wavy interrupted lines or narrow bands,
like the edges of compressed cups of Fenestella in the Carboniferous
Limestone*, and on breaking open the rock, I found them to be
similarly due to undulating sheets of Fenestella, or of some closely
allied form.

The cleavage of the rocks from Lynton to Heddons Mouth dips
everywhere south or south-south-east, usually at an angle of 50° or
60°; but in two places, where the beds were horizontal, I find it
recorded in my note-book as dipping at as low an angle as 15°.
The beds at Heddons Mouth dip south at 20°; east of Woodabay the
angle increases to 30°, but as the shore bends to the north, the angle
flattens to 15° and 5°, and just west of Lynmouth the beds are
horizontal. I did not visit the headland east of this, under Countes-
bury, but from the deck of the steamer the beds seemed certainly
to dip at a high angle to the north, as drawn in Sir H. De la
Beche’s sketch-section in the Report on Cornwall, Devon, and West
Somersetshire.

Proceeding inland the beds undulate at gentle angles, as may be seen
in the valley of the Hast Lyne and elsewhere. A little farther south,
however, there appears to be a higher northern dip. Greenish-grey
grits and gritty slates dip north-west at 45° in the bed of the brook
near Sparhanger, and bluish grey slate and brown grits dip north-
north-west at 20° in some quarries near Brendon. If the rocks rise
to the south persistently for any distance south of this, the top of the
Old Red Sandstone will probably reach the surface. I did not see any
rock for some miles to the southward, except one small quarry near
Farley Common, where a brownish sandstone dipped south-west at30°.

* Mr. A. B. Wynne, now of the Indian Survey, first called my attention in

Treland to the fack t that, these wavy markings were the edges of undulating sheets
and cups of Fenestella.

1866.] JUKES—OLD RED SANDSTONE AND DEVONIAN. 303

wi This sandstone might be either
part of the Old Red Sandstone
or a Coomhola grit. No rock
was to be seen for three miles
south of this, on or near to the
road to Simonsbath, until I came
to a place where the road crossed
a little rocky ravine with a small
brook, which the driver declared
was the head of the Exe *.

Simonsbath,”
River Barle

"5 OOFT The rock shown here was a
8 bluish-grey, shining, clay-slate,
ae precisely like some parts of the
‘a Carboniferous Slate of Ireland,
Z which appeared to dip south at

10°. Near Simonsbath similar
slate, but paler, appeared to dip
south at 30°. At both places the
cleavage dips south at 70° or 75°,
and as there were no decided grit
bands, and no layers of fossils,
or any appearance of fossils at
all, it was with some doubt that
I decided on the dip of the beds.

The section in fig. 12 will show
the above facts in a diagram-
matic form, starting from a point
a mile east of Lymmouth and
crossing the country to Simons-
bath.

The green little open valley
of Simonsbath was very similar
in aspect to valleys in the Car-
boniferous Slate in Ireland, and
I greatly regret that I was un-
fortunately prevented from re-
turning here, as I intended, to
trace the Barle down to the part
where it runs in a deeper and
wilder glen through the Old Red
Sandstone north of Dulverton ;
for it is there that I should most
hope to find sufficient exposures

Dure Down.

Length of the section about seven miles.
The rocks near the coast at the north end of the section as far as Brendon are dark-grey slates and grits (lower part of the Carboniferous

Fig. 12.—Section Lynmouth to Simonsbath.

In the other parts nothing was seen.

*, Brendon.

East
Lyne
Ao

* The people at Simonsbath assured
me that this was the place called

TOA

Those about. the heads of the rivers Exe and Barle are dark-grey slates without grits (higher parts of the Carboniferous Slate).

The sandstone near Farley is doubtful.

aed EA: Prayway, which, on the Ordnance

-duep —__ + As map, is placed at the head of another

3 : a stream. The map was, indeed, nearly

2b 3 useless here, as neither the roads, ri-

wena cia R vers, nor features of ground marked
°

on it agreed with the existing ones.

3bo4 PROCEEDINGS OF THE GEOLOGIGAL SOCIETY. [Mar. 7,

of rock to enable one to observe directly the relations of the rock-
groups to each other.

Returning to Lynton I collected a few fossils in the grey calcareous
grits on each side of the Valley of Rocks, and snatched rather than
collected some blocks full of fossils from a set of fragments that had
slipped from the cliffs above into the valley of the East Lyne. I
believe the fossiliferous beds near the hill-tops of the valley of East
Lyne to be very nearly on the same horizon with those of the Valley
of Rocks, and to be above the hard siliceous grit-band mentioned
above as exposed in the road cuttings down from Lynton to Lyn-
mouth ; so that fossils may probably be found almost everywhere in
the upper part of these hill-sides. I found them certainly at several
places in the lanes and fields above Lynton, south of the Valley of
Rocks, in grits that weathered to a reddish brown.

These fossils were examined by Mr. W. H. Baily, and Mr. David-
son was also kind enough to look at the Brachiopoda for me. On the
authority of those gentlemen they contained the following species :—

Fenestella antiqua. Spirifera speciosa, var. paradoxa.

Athyris concentrica. Streptorhynchus crenistria ? or umbra-

Chonetes sordida*. culum.

Rhynchonella, sp. ? Pleurotomaria aspera.

Spirifera aperturatat ? or caudifera. Actinocrinus(o7 Cyathocrinus) variabilis.
hysterica ? Cyathocrinus ellipticus.

—— levicosta (ostiolata, Schlot.). Phacops latifrons.

There is one little quarry on the hill-top, south of the Valley of
Rocks, near where a small tumulus{ is marked on the Ordnance
map, in a grey and reddish mottled calcareous-looking rock, which
is full of fossils, especially Fenestella and a small Orthis or Chonetes.
The beds in this quarry dip south at 30°.

6. Lynton to Ilfracombe.—Proceeding from Lynton to Ilfracombe, I
was again disappointed in my expectations of seeing new quarries or
cuttings on or near the road, which keeps as much as possible on the
high ground. As before, near Exmoor, this high ground shows a
gently undulating dreary-looking expanse, rising into continuous
moorlands towards the interior, and ending in lofty cliffs along the
coast. The unbroken outline of the moorland: watershed, and the
gradual increase in the number and depth of the gullies and ravines
that run off on either side of it, attest the influence of the rain, and
its resulting rivers, in carving out all the picturesque features of the

* Mr. Davidson seems to be of opinion that this is only a variety of the Car-
boniferous species, Hardrensis (Devonian Brach. p. 94).

t [Fragments and imperfect casts of a large Spirifera, with irregular and wide
ribs, beautifully covered with very fine, close, concentric lines, which Mr. David-
son says he could not determine to his satisfaction ; adding that it is probably to
a fragment of this shell that Phillips applied Schlotheim’s term Spirifera aper-
turata (Pal. Foss. Cornwall, &e. p. 77. pl. xxx. fig. 133). See also Mr. Davidson’s
remarks, at_pp. 26 & 116 of his “ Devonian Fossils” in Mem. Pal. Soc.).] Note
by Mr. Baily.

¢ Curiously enough I found this tumulus to be, not a regular conical mound or
cairn, like those which are common in Wales and in many parts of England, but
a circular rampart, exactly like the ‘ Raths” scattered over the south of Ireland.

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN, 355

country. Had the ravines been in any way due to internal disturb-
ances and dislocations (a belief which still seems to linger in the
minds of some geologists of eminence), why did not some of them
cause at least one ravine to cross the present watershed? The rocks
must be as much disturbed about the watershed as anywhere else,
according to any hypothesis as to the internal structure of the
country ; but the surface is an unbroken, gently undulating, upland
plain or moor.

There is one quarry on the left of the road, about a mile south-west
of Parracombe, near the hill-top before reaching the turnpike, which
showed a glossy-black slate with some dove-coloured sandstones,
over which were some black, earthy, carbonaceous-looking slates,
all dipping south at 30°. I was half inclined at first to look upon these
as possibly the base of the Coal-measures rolled in, as a small basin,
but was unable to find any fossils in them. Subsequently I saw
beds like the grits near Ilfracombe.

Going down the hill into Ilfracombe I again examined the quar-
ries which had formerly puzzled me; but was again baffled, and
unable to come to any decided opinion as to the dip of the beds. A
very strong cleavage dipping south at a high angle, obliterates the
stratification.

Walking to the east, however, from Ilfracombe as far as the
bathing place called Rapparee Cove, and thence over the hill to
Helesborough, I met with rocks of unmistakeable characters. The
dark slates with occasional grit-bands are precisely those of Kinsale
Harbour, for instance, or of so many other places in County Cork.
These slates lie higher in the series than those in which the Coom-
hola grits occur. The grits they do contain are usually in single
beds and are unfossiliferous. The slates, too, are often unfossiliferous
in Ireland through a thickness of one or two thousand feet and an
extent of many miles. The general dip of these rocks, east of Ifra-
combe, is certainly to the south, at angles varying from 30° to 60°,
but this dip is by no means so persistent as it at first appears.

As it is possible that some young geologist, unaccustomed to cleavage in rocks,
may visit this spot, perhaps I may be pardoned for entering a little into details
which may serve to guide his observations.

Keeping along the south side of the harbour towards the bathing-cove, which
the boatman called Rapparee Cove, he will see a limekiln, near which there is a
little cavernous hole under the cliff.

The arched roof of this little cavern nearly coincides with a curve in the beds,
as shown by the narrow bands, differing slightly in colour and grain (the
“stripe’’ of Professor Sedgwick), which indicate the original bedding of the
rock, The cleavage, however, dips steadily to the south at 66° (see fig. 13).

A still more striking example presents itself in Rapparee Cove. This is a
small pebbly cove, some 50 yards across, surrounded, except at the seaward
opening, by vertical cliffs 40 or 50 feet high. The rocks are dark-grey slate,
with two single beds of grey grit appearing in the western cliff, both dipping
steadily to the south at 50° or thereabouts. This dip is so obvious that an
observer might readily be pardoned who entered it in his note-book as the dip
of the whole mass of rock, and allowed it to form an element in his calculations
for the thickness of the group. I was at first doing so myself; and had there
been a path out of the cove to the eastward, might have been satisfied with the
_ observation, and passed on. The only entrance to the cove by land, however, is

306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

by some steps cut in the cliff, near the foot of which is a wooden bathing-house ;
and on returning towards the steps my attention was attracted by a sharp little
ridge of gritstone that rose up from among the pebbles on the floor of the cove,
and ran towards the northern corner of the bathing house.

e

\
| NS

\ \
x

re. Yaa
i NN WS

Small cavity near limekiln, half a mile east of Ilfracombe, showing contorted
beds traversed by slaty cleavage.

Small Anticlinal ridge in Rapparee Cove, near Ilfracombe.

This little ridge of grit had a steep face to the north, on which was a well-
developed “ripple” or “current-mark.” As this could have been formed only

1866. ] JUKES—-OLD RED SANDSTONE AND DEVONIAN, 357

on the upper surface of the bed, I saw at once that the little ridge was the top of a
sharp anticlinal fold, of which no trace appeared in the cliff of slate above it.
Neither was this the only one, for some other crumpled grits showed themselves
a little farther south, on the floor of the cove.

These undulations greatly reduced the thickness, which the appearance of the
two grit-bands on the western cliff, dipping steadily south, and so far apart from
each other, would have led me at first to assign to the rocks shown in the cove.
Nor was this all, for on looking more attentively I found that the two grit-bands,
which seemed to strike so steadily towards the east in the western cliff, did not
appear in the eastern cliff of the cove at all, but were cut off by some fault or
“trouble” at the south-east corner of the cove.

The western cliff was formed wholly of slate, which might at first sight be
supposed to dip south, but did in reality undulate in various directions, and was
in some places horizontal. This was shown by the little parallel bands of dark
and light-grey colour, about one-tenth of an inch wide, producing what we call
“‘ribboned slate” in Ireland. They were traversed by a well-marked cleavage,
which dipped south at 60°, and one set of joints was parallel to this cleavage, pro-
ducing exactly the appearance of bedding, so that any observer who was not
greatly on his guard, might easily have been deceived, by the facts observable in
a cove, into assigning a steady persistent southern dip to the whole of the

eds.

From what I saw elsewhere about Ilfracombe and Mortehoe, I believe that,
while there is a real general dip to the south throughout the district, this dip
is by no means so prevalent as it appears to be, and that the total thickness
is accordingly much less than would be at first supposed.

In the little cove of Helesborough, about a mile east of Ilfracombe,
the slate contained in one place a strong calcareous band, consisting
of nodular lumps of white calc-spar, weathering brown, with strings
of the same substance ramifying into the grey slates. The dip here
is certainly south-south-west at 35°.

7. Pickwell Down and Mortehoe.—Proceeding from Ilfracombe to
the south-west by Bicklescombe and Score (? Scaur), and thence along
the lanes towards Pickwell Down, nothing was to be seen, before
reaching Crosscombe, but small quarries and cuttings in dark-grey
slate, apparently without any grit-bands. It would have been
quite useless, therefore, to waste the little time at my disposal in
attempting to determine the dip of the beds. The cleavage still
dipped everywhere to the south at 60° or thereabouts. At Cross-
combe, however, I came on a little quarry in thick, coarse, brownish-
red sandstone, with slaty partings, some of which were a dirty
yellow, and some of a bright-red. “Genuine Old Red Sandstone ” is
the note I find in my note-book as to these beds. They dip 8S. 10°
W. at 45°.. From this quarry, for a mile and a halfto the southward,
over Pickwell Down, there is no rock exposed in situ, that I could
find, except in shallow little quarries that did not go deep enough
to show the “lie” of the rock. The fragments in these quarries,
the field-walls that had been built from them, and the angular
rubble and pieces covering the ploughed fields and stubbles, con-
sisted chiefly of yellow and red gritstones of various shades, from
light yellow to dark brown, and from light pink to deep claret-
colour. Some pieces of purple slate, or of yellowish-green slate
also occurred. 7 ae

_ I walked over the seaward slope of Pickwell Down, hoping to
find some natural or artificial excavation that would disclose the

358 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 7,

rocks, but in vain. The beach is backed by lofty sand-dunes piled
against the foot of the Down. Nothing seemed to be shown before
reaching the farm called “ Vention,” where I had previously seen
rocks identical in character with the upper part of the Old Red
Sandstone of county Cork (see Journ. Dublin. Geol. Soc. vol. x.).

Taking, however, what I did see in connexion with what I had
previously seen, north of Braunton, on the road from Barnstaple to
Ilfracombe, near Span Head, and north of Dulverton, I can have no
hesitation in affirming the existence of a band of Old Red Sandstone
striking from Morte Bay, for a distance of about thirty-five miles
into the country, with a general dip to the south, at a very high
angle.

The surface-width of this band appears to be about two miles;

and if we estimate its average dip at 40°, it will give us a thickness
of about 7000 feet. It is, however, quite possible that undulations
in the beds, if we could see them, would greatly reduce this amount,
and that the actual thickness of Old Red Sandstone which reaches
the surface may not be more than half that calculated above.
- Walking along the beach toward Tracey, I found some crags in
situ on the beach, and also in a quarry in the side of the lane going
up to Pickwell Down. These are, about “ Potter’s Hill,” as marked
in the Ordnance map. The crags on the beach are described in my
note-book, as “‘pale-grey grits and slates, dipping south at 70°, cleavage
perpendicular, with nodular*bands, as if calcareous, but I believe
ferruginous (?).. Are these Carboniferous Slate or Old Red Sand-
stone?” ‘The quarry up the lane is described as showing “ softish
purple and green sandy slate, dip (?) south at 70°.” These beds are so
very indefinite in character that I must frankly give them up. They
might possibly be deep in the Old Red Sandstone, or they might
be part of the Carboniferous Slate.

North of Tracey, however, where the rocks are well shown on
the coast, and thence to Mortehoe, and down again into Lee Bay,
all the rocks are identical in character with parts of the Carboni-
ferous Slate of co. Cork, such as are shown about Bandon and
Kinsale, or about Rosscarrberry, or between that and Dunmanway.
There are scarcely any grit-bands, the whole mass being a smooth,
shining clay-slate, black when fresh and damp, but weathering to a
pale greenish-grey. It all seems at first sight to have a steady dip to
the south. The cleavage certainly does dip steadily at 50° or 60°,
but the more I worked with the hammer at the slate rocks near
Mortehoe, the less persistent appeared to be the dip of the beds.
Over large spaces I could not succeed in bringing out any structure
that could be depended on as the stratification of the rock. On
some parts of the low rocky cliffs near Mortehoe, the true bedding
of the rocks coincided with the cleavage. In other parts the beds
dipped northwards, while the cleavage dipped south. This was cer-
tainly the case near a place called “ Yard,” about a mile north-east
of Mortehoe.

While, then, I agree with all previous observers in assigning a
general southern dip to the whole of the rocks of North Devon, and

1866. | JUKES—OLD RED SANDSTONE AND DEVONIAN. 359

believe the Mortehoe, Simonsbath, and Exton slates to be above
those of the Lynton district; I believe that it is next to impossible
to assign a thickness to the former with anything like the approxi-
mation to certainty we might possibly do to the latter, and that
their apparent may be vastly in excess of their real thickness.

In making observations on the dip of the beds in a great section of slates,
even the most practised observers may be occasionally led astray.

If the beds undulate while the dip of the cleavage is steady, and if the sub-
stance of the slate be very homogeneous, it may easily happen that the stratifi-
cation is only well shown when it has a given relation to the cleavage, when for
instance they coincide, or when they are at right angles to each other, or when
they cross at some other angle, so that the particular mark of stratification which
the kind of slate possesses shall be least obscured by the cleavage. But, when,
in observing a long section, a number of these comparatively well-marked “dips”
occur at several intervals, all in the same direction, an observer is apt to sup-
pose that the intermediate parts dip also in the same direction, and base his
estimate of thickness on the width of the whole mass and its mean angle of in-
clination. It is possible he may be right, but it is also quite possible that he
may be wrong; and that the section may only show the same comparatively
small group of beds undulating across it, as suggested in fig. 15, where the parts
showing the bedding distinctly are supposed to be those which coincide with

the cleavage.
.s
oo
aK N WONG (NW \ \ \

N. Fig. 15.

\ AAA \W AW FATA
— AN i Kt ni

\ \ \ \
AN nd MANA

@, b, c,d. Places where the stratification coincides with the cleavage, and is there
observable, while in the intermediate places it is not discernable, or vice versd.

If in such a section the bedding were
well seen at a, 6, c, and d, and not at all
observable in the intermediate parts, the
whole mass might be supposed to dip
south at 45°, and show a continuous suc-
cession of beds, instead of a repetition of
the same.

While on the subject of cleavage I
may perhaps be allowed to mention a
structure I observed at Mortehoe, which
I took at first for stratification, but had
afterwards reason to doubt it; I have
often observed it before, and it is some-
times very deceptive, and may accord-
ingly lead to very erroneous conclusions.
Along certain parallel bands in the slate,
about 1 inch in width, and a foot or two
apart, there occurs a shake or crumple
in the cleavage-planes. Viewed in sec-
tion it would be as in fig. 16.

It is, however, when observed on the
face of a bed that it is most deceptive,
as the change of tint resulting from the
difference in the angle of reflection of
the light gives to the little bands the ap-
pearance of a difference of colour in the
substance of the rock, so that they might
be taken for the true “stripe” of the slate.

360 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 7,

8. Aspect of the Country.—In tra-

t versing the country between Morte-
j hoe and Lee Bay, I was again struck
¢ with the exact similarity of the form
(e)

° 3 of ground and nature of scenery to
2. 3 that so frequent in the Carboniferous
SES n Slate country of county Cork. The
SO oS & 3

As 2 general surface of the high ground is
b¢ = uniform and monotonous, but it is
pe fo) cut into such numerous little dells,
3 SS opening out into deeper ravines, and
& these into steep-sided, flat-bottomed

valleys, that it becomes picturesque
and beautiful. The tops of the hills,

3 too, left standing between the ravines
3s g and valleys, are varied by frequent
= 8 little brows and ridges of slate, form-
Q 3 ing small, parallel, escarped terraces,
Ss $& and rocky crags, and furze-covered
Sh S83 kmolls, while the colour and nature
a “¢® of the soil, and all the minuter fea-
3 2 3 tures of the scenery are identical in
oo 84 p24 both countries.
ages g3 T was hastily summoned from II-
3 AA Sf fracombe, on private business, before
BS Rie x I could examine the calcareous bands
3 88 “~~ and other rocks of Combe-Martin and
a its neighbourhood. If, however, the
Sis # Lynton rocks below, and the Ilfra-
> 2 a combe and Mortehoe rocks above be
= aS determined, the intermediate Combe-

; ‘= ~=©6 Martin beds follow as a matter of
i "% ~—«- course.

bs o 9. Probable Existence of a Great
° East and West Fault with Downthrow

8 to the Northward.—Having now laid

S before the Society the means I have

a had of examining the rocks and form-

ing an opinion upon them, I have to

state my deliberate judgment that

; the rocks of Lynton, Ilfracombe, and

: g. Mortehoe are part of the same group

ie 2 of rocks as those called the Carboni-

eg E ferous Slate in Ireland, and that the

at ae rocks which strike from Pickwell

oe. 8 Down, through Swinham Down, Gar-

<i iy af monds Down, Span Head (of the Ord-
Sa. Gokee ees = nance map), and Dulverton Common,
aa to Haddon Down, are the upper part

Zi of the Old Red Sandstone of Ireland ;

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 361

the Irish Old Red Sandstone being the same as that of South Wales,
but more indurated and traversed by slaty cleavage. If that judg-
ment be a correct one, it follows, that as the Carboniferous Slate of
Ireland is, without doubt, above the Old Red Sandstone, the Old
Red Sandstone striking from Pickwell Down to Haddon Down will
be below the rocks of Lynton, all appearances to the contrary not-
withstanding ; and that consequently some great fault, with a down-
throw to the north, must run between the two, as suggésted in
fig. 17. The alternative to the conclusion will be, that there is a
band of rocks, from 3000 to 7000 feet in thickness, precisely ‘re-
sembling the Irish Lower Group, but lying in Devonshire in the
middle of the Upper Group. If there were any direct evidence in
Devonshire that such is the structure of the country, all that could
be said would be, that it was a very remarkable, and, as far as L
know, unexampled occurrence. There is, however, no direct evi-
dence for it beyond the general southern dip of the country, which
is just as compatible with one hypothesis as the other. There is no
place that I could find, either by my own search, or described in any
published researches of others, where the band of slates stretching
from Mortehoe to Exton can actually be seen to pass under the red
sandstones and slates that stretch from Pickwell Down to scabies
Down; they can only be seen to dip towards them.

10. Thickness of the rocks of North Devon on the ordinary hi ees
thesis.—There is even a strong presumption against the ordinary
hypothesis to be deduced from the enormous thickness which it com-
pels us to assign to the rocks of North Devon, and that without
arriving at any definite base to them. All observers, from Sedgwick
and Murchison, Weaver*, De la Beche and Phillips, down to our
own day, when the Rev. M. Mules, of Marwood, and my colleague,
Mr. Etheridge, who have constructed rough maps of the country ft,
and Mr. Townshend M. Hall, of Pilton, who has described it to the
Exeter Naturalists’ Field Clubt, agree in the opinion that there is a
regular succession of rock-groups, dipping one under the other, from
Lynton to the latitude of Barnstaple Estuary and South Molton.

Mr. Weaver, the accuracy of whose observations no one has ever
disputed, divides the rocks of the country into eight such groups, as
follows :—

. Culmiferous Shales.

. Wavellite schistus and limestone.

. Trilobite slates.

. Woollacombe sandstones, flags, and slates,

. Morte slates.

. Trentishoe quartzy-slate and sandstone, including the
Combe-Martin limestones.

. Lynton calcareous slates.

. Foreland sandstones (top of Old Red Sandstone ?).

* See Proceedings of Geol. Soc. London, vol. ii. p. 589, Jan. 3rd, 1838.
t I am indebted to both these gentlemen for a sight of these maps.

+ Reported in the Exeter and Plymouth Gazette, Sept. 29th, 1865.
Yor. XXII,—PART I, 2¢

} Coal strata,

CS = Or Oo NT OC

mt bo

362 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. %,

The two uppermost of these groups, Nos. 7 and 8, belong to the
Coal-measures, the other six are the rocks subsequently known as
Devonian; and he says, they form “one persistent consecutive
series,’ all dipping generally to the south, with a few occasional
undulations. The angle of dip, he says, increases from 20° on the
north to 80° on the south, being from 20° to 30° in his Ist and 2nd
groups, from 45° to 70° in his 3rd group, and generally 80° in his
Ath, 5th, and 6th; a“‘lower angle being sometimes observable on
approaching an undulation”*.

All the published accounts, so far as I am aware, have a eerie
agreement with those statements, and I should myself agree generally
with them so far as they profess to be descriptions of observed facts.

Now the distance in a straight line, measured directly across the

strike of these beds, from Lynton to South Molton, is about fourteen
miles, or 73,920 feet. If we say 70,000 feet, and assign a mean
angle of inclination of 45° to the dip of the beds, we get a total
thickness of 49,490 (say 50,000) feet for them. But suppose we
deduct about a third of the width as an allowance for undulations -
in the beds, and reduce it to 50,000 feet, and allow the mean angle
of inclination to be only 30°, and I think the observable facts will
hardly admit of any greater reduction on the hypothesis of a suc-
cession of consecutive groups, we must still believe that the beds
below the Coal-measures in North Devon have a thickness of 25,000
feet, and that without reaching their base, which is concealed some-
where under the waters of the Bristol channel.

It appears to me that this is a result that requires a comparison
with some other district where these same rocks can be measured,
either for its correction or its verification.

Comparing them with the south-western part of Ireland, the cor-
rection I propose is the inevitable result.

It detaches the true Old Red -Sandstone from the grey-slates,
which contain marine fossils, and‘thus divides the thickness, in the
first instance, between two distinct formations, while, with respect to
the grey slates themselves, it shows those of one district to be a re-
petition of those of the other, and therefore that the thickness of
one is not to be added to that of the other.

The structure of North Devon, then, will be represented by the
figure 17, in which the facts observed in different parts of the
country are grouped together and condensed. It does not, then,
represent any particular line of country, but offers a key to the
structure of the whole.

The structure is that of a broken: anticlinal, the northern arm of
which has sunk in against the southern arm; the line of fracture
running along the crest of the curve. It is by no means an un-
common structure. There is an excellent example of it in the hill
of Shevnamuck, in the county Tipperary, where in ike manner the
northern arm of one of a series of parallel anticlinal ridges has
fallen in against the southern arm. In that place a thickness of
700 or 800 feet of Coal-measures is brought in direct apposition with

* Proceedings Geol, Soc. London, vol. ii. p. 589.

1866.] | JUKES—OLD RED SANDSTONE AND DEVONIAN. 363

the Lower Silurian Rocks. There are places there, where in an
open ditch, it is possible to stand with one foot on Lower Silurian
slates, and the other on a bed 700 or 800 feet above the base of the
Coal-measures. ‘To the north of the fault several beds of Coal-mea-
sures may be seen, in many places, cropping out on the slope of the
ground; while still farther north a great tract of Carboniferous
Limestone rises out from below them, across which it is necessary
to travel for some miles before the Old Red Sandstone rises up in the
ridge, near Emly. To the south of the fault, on the other hand,
the base of this Old Red Sandstone may be seen reposing on the
highly inclined Silurian slates; and the hill above shows several
hundred feet of it, the beds dipping south, under another Carboni-
ferous Limestone valley, the beautiful Vale of Aherlow. ‘The
Shevnamuck fault, then, must have a downthrow to the north of
at least 4000, and possibly 5000 feet. (See Explan. of Sh. 155,
Geol. Surv. Ireland, or ‘ Student’s Manual,’ p. 286.)

A similar throw in the supposed fault in North Devon would
account for all the observed facts.

11. Objections considered.—The arguments against the hypothesis I
propose, may be arranged under three heads, (a) stratigraphical, (6)
lithological, and (c) paleontological.

a. The stratigraphical objections have already been sufficiently con-
sidered, and it has been shown that while the observable stratigra-
phical facts would not of themselves lead to the hypothesis, there are
none which are conclusive against it. I may also state my belief that
it would inevitably have occurred to any one who had examined North
Devon, after having made himself acquainted with the structure of the
south-west of Ireland. Had it so happened, for instance, that my
old teacher, Professor Sedgwick, and my present chief, Sir R. I.
Murchison, had been familiar with the rocks of the county Cork
before entering on Devonshire, I believe they would have announced
the existence of this great fault as a matter of course.

6. The lithological arguments against the hypothesis seem at first
to be stronger. The aspect of the beds about Baggy Point, Barn-
staple, and Dulverton is not exactly the same as that of the Lynton,
Ilfracombe, and Mortehoe beds ; and the limestones of Combe-Martin,
&c., appear from published accounts to be stronger than the thin
bands of calcareous slates in the Barnstaple district.

In reply I would urge that the Carboniferous slate of Ireland
varies in character in different districts to such an extent that its
parts might not be recognized as belonging to the same formation, if
their physical continuity could not be traced, and their different

_ graduations followed across the country.

In Devonshire itself the beds which dip under the Coal-measures
on the north, differ in aspect from those which rise from under those
same Coal-measures on the south, although they must be on the same
general horizon. 'The limestones which prevail near Combe-Martin,
and in South Devon, are local banks of limestone, which did not
happen to be formed in the beds about Barnstaple and Dulverton,
though the calcareous matter is not totally absent there.

2c2

364 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

The sandstones, both in Ireland and in North Deyon, which
are interstratified with the grey-slates, vary greatly in thickness.
Near Bantry the Coomhola Grits are 3000 feet in thickness; in
many places near Cork 20 or 30 feet is the maximum that could be
assigned to them, and they have no greater thickness at Kenmare,
which is not more than ten or twelve miles from Bantry Bay. That
similar variations in the thickness of the sandstone beds, and. their
mode of interstratification with the slates should occur in Deyon is
only what is to be expected. I would also remark, that though
there is not a minute lithological identity between the beds of the
Baggy Point country and those of the Lynton district, there is after
all no very great difference between them; alternations of greenish
and greyish grits, with grey slates, prevail in both cases ; and if the
‘lie of the beds,” and their circumstances of exposure were alike,
I believe their similarity of aspect would appear greater.

The objections, then, arising from variations in lithological cha-
racter in different localities a few miles apart cannot be accepted as
valid against the supposition that they belong to the same group of
beds.

c. The paleontological resemble the lithological objecnans and.
allow of a similar answer.

There are fossils in the Lynton and Combe-Martin district which
are not known in the Baggy Point and Barnstaple district, and vice
versd; but there are also fossils which are common to the two dis-
tricts. If the lithological variations are admitted, some paleeonto-
logical difference may be expected to follow as a matter of course.

In Ireland, where the Carboniferous Slate forms one physically con-
tinuous area, and where its lithological structure is simpler than in De-
vonshire, many fossils are peculiar to parts of that area, some species
only occurring in one or two localities. (See Mems. of Geol. Survey,
Explanations of sheets 187, &c., and 192, &c. of the Irish maps.)

It may, then, be reasonably expected, even when all the species
are collected, that different species will occur in the same beds in
different parts of Devonshire. I refrain from entering into a discussion
respecting species of fossils in which my own knowledge would not
allow me to take any part except at second-hand, but I may be al-
lowed to mention the following list of species which I find given
by paleontological authorities as common to the districts north and.
south of the central band of Old Red Sandstone in North Deyon.

Species. South. North. Authority.
Cyathophyllum (Zurbinolopsis, : +77:
y ree L ig) plusiradiale... - ~’| ¢ Brushford ...) Lynton ......... Phillips.

Palo: wate vate Lynton ...... lay

Fenestella antiqua ......s0s..000 Croyde.cc,. cae: Mee’, Ce: eae vy
Brushford ...) Woodabay .. “|

Actinocrinus tenuistriatus...... Piltorticccaceeeaes iyntona.. cee :

Cyathocrinus variabilis ......| Pilton............ Haymtion i asewont ds

Pleurotomaria aspera ......... Paton .cpicececes Woodabay....|

1866. ] JUKES—--OLD RED SANDSTONE AND DEVONIAN, 3690

Species. South. North. Authority.
Piltomisee. a2:
Bellerophon globatus......... és | Brat me ponds . .|Phillips.
Marwood......
Athyris concentrica ....+....... PiltOms. cs cgecw hes Ilfracombe.....| Davidson.
Barnstaple, 7
Chonetes Hardrensis.........../4 Braunton Lynton o«... =
Marwood
. Barnstaple ...| | Haggington
Orthis interlineata............... Croyde ‘ | Hill, near =i
Marwood.....| } Ilfracombe ..
PRECUUNG cases cevicsctessyes Pilton Jo. .c5-useet Ilfracombe ..... .
Rhynchonella pugnus ......... Pilton: (2 aides: Ilfracombe..... ‘
POUPOCOI .\). accesses sos: PiltOnisaec:teaeans| DMradombe «i. 3
Spirifera lsvicosta vel ostiolata| Pilton...,........ Py Htorl wasaaesa: 3
Spine erty 807 C2 ion ee] Ltecomberee|
Barnstaple ..|] Haggington | \
Strophomena rhomboidalis* |} Braunton .. } Hill, near { .3
Marwood...... Ilfracombe ...
Streptorhynchus crenistria { StS Tifracombe..
***| | Barnstaple ... ifs ii
| fhacops latiironst .........| Braunton ......| Lynton ....,.... Baily. |

I may be pardoned, perhaps, for anticipating a considerable ac-
cession to this list when a thoroughly exhaustive search has been
applied to the country t.
~ 12. Considerations on the Devonian Fossils.—As many persons will
be inclined to place great reliance on the Devonian fossils as fixing
the place, or the age, of the Devonian rocks, it is advisable to deter-
mine the precise value of this evidence.

In the first place, I would remark that the problem to be solved is
restricted within narrow limits. The question is, to which of the
two conformable groups of beds—the Carboniferous Limestone or
the Old Red Sandstone—do the Devonian beds belong?

* Strophomena depressa (formerly Leptena and Producta depressa), and S+
rugosa and analoga are now included under 9S. rhomboidalis, by Mr. Davidson.

t Specimens of this trilobite were procured by me from the late Mr. Symonds
of Braunton, and collected by myself at Lynton last year; it occurs also at
Pilton and elsewhere.

{ This anticipation has already been partly verified. In the number of the
‘Geological Magazine,’ for April last, was a letter from Mr. Spencer George
Perceval, of Severn House, Henbury, Bristol, giving an account of some fossils
he had found near Witthycombe, a couple of miles south of Dunster. The beds
_ are an extension of the Combe-Martin beds, but not only do they contain,
according to Mr. Perceval’s determinations, at least fourteen species of Devonian
corals, but a large species of Cucullea, together with Terebratulz, Spiriferee, &c.
It will be interesting to know whether this Cuculiea is the same as one from
Marwood or Braunton, or is the Cucuilea Griffithii of Ireland.

I would also beg leave to take this opportunity of asking Paleontologists
whether there is any great difference between the Myalina from the Carboniferous
rock of Scotland (Carluke and Pitlossie), and that from Hangman Hill, near
Combe-Martin. Both specimens are in the Museum of Practical Geology in
Jermyn Street, (Note added in July as the paper passed through the press.)

366 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

Had the Devonshire slates contained Silurian fossils:‘on the one
hand, or Lias fossils on the other, they would, as a matter of
course, have been referred to the one or the other of those two for-
mations.

The choice now, however, is limited to the period of the Old Red
Sandstone and that of the Carboniferous Limestone, unless we as-
sign to them a hitherto undefined period between those two, or sup-
pose them to be older than the Old Red Sandstone.

We need hardly trouble ourselves, however, with the two latter
suppositions.

Now, the Devonian fossils are said to comprise some species
which are found also in Silurian rocks *, and are not known in the
Carboniferous Limestone. They undoubtedly contain many spe-
cies found in the. Carboniferous Limestone + which are not known
in any Silurian rock, as well as a few (such as Strophomena rhom-
boidalis), which range from Silurian into the Carboniferous Lime-
stone.

The Devonian fossils also comprise some peculiar species of Silurian
genera, which do not occur as species in Silurian, nor as genera in the
Carboniferous Limestone. Some of the Trilobites are conspicuous
examples of this case.

They also comprise some peculiar species of Carboniferous ge-
nera (Producta, for instance) which do not occur as species in Car-
boniferous Limestone, nor as genera in the Silurian rocks.

Lastly, there are some genera (such as Stringocephalus among the
Brachiopoda, Megalodon among the Conchifera, and Calceola, what-
ever that may be) which are peculiarly Devonian genera.

Altogether, the Devonian fossils have an intermediate aspect

(whether in the specific characters of some, as pointed out first by
Mr. Lonsdale, or in their general facies) between those of the Upper
Silurian rocks and those of the Carboniferous Limestone,
_ The natural presumption, therefore, was, that the beds contain-
ing those fossils were intermediate in age, and therefore contempo-
raneous with the Old Red Sandstone, which could be observed stra-
tigraphically to hold that intermediate position.

However natural that presumption was, however, I ae be per-
mitted to urge that it was a presumption only, and not a proof.

The intermediate biological character of the Devonian fossils, to
whatever extent it may exist, is neither a conclusive proof that they
are of the age of the Old Red Sandstone, nor that they were not
contemporaneous with those in the Carboniferous Limestone.

The geological age of fossils is proved by the stratigraphical po-
sition of the beds containing them. When that age has been
established by reference to clear sections in one or two localities,
the fossils themselves are admitted as evidence of the age of beds
in other localities whose stratigraphical position perhaps is not
clear. In all such cases, however, there must be either an ayowed

* Mr. Etheridge reckons these as 13, mostly Corals.
t+ Mr. Etheridge reckons these as 92.

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. 367

or tacit reference to sections in the first instance, showing the
stratigraphical relations of the beds.

It may be reserved for some future paleontologists to treat fos-
sils independently, and show, from their biological relations only,
the necessary laws which must have regulated their appearance in
time ; but I am not aware of any one haying even attempted this
task as yet.

To take an extreme case at once, the family of the Graptolitide
for instance: if any geologist now find in any rock a fragment of
a Graptolite, he refers the age of that rock to one of the Lower
Paleozoic periods with the utmost confidence, and in no known in-
stance would he be wrong in so doing. But he does so, not because
of anything in the organic structure of the fossil, but because no
one ever yet did find a Graptolite in any rock which could be
shown stratigraphically to belong to the Upper Paleozoic or any
higher part of the series. No paleontologist, so far as I am aware,
could show a merely biological reason why the Graptolites might
not have existed during the Secondary or Tertiary epochs. Or
suppose that no shells belonging to the genus Producta had ever
yet been seen, could any one on the first discovery of a Producta
have decided on its age without any reference to the stratigraphi-
cal position of the bed in which it was found? ven if he had
guessed, from its biological relations to other Paleozoic Brachiopods,
that the shell was itself of Paleozoic age, still he must have based
his conclusion on the fact that those other Brachiopods had hitherto
been found only in beds which were shown to be of Paleozoic age
by their stratigraphical position.

The very value of the doctrine of the chronological significance
of organic remains, and the constant use made of it by geologists,
seem sometimes to have caused them to forget that the significance
is a secondary and derivative one only, depending, either directly or
indirectly, on the stratigraphical succession of the beds in which the
fossils are to be found, and upon that alone.

The peculiar Devonian species and genera of fossils, therefore, have
no definite value in themselves as fixing the exact place in the series
of the rocks in which they occur, until the place of those rocks has
somewhere been determined by stratigraphical evidence. Those
rocks have of late years been held to occupy the same place in the
series as the Old Red Sandstone, or to lie between the top of the
Upper Silurian and the base of the Carboniferous Limestone; but.
where, in England or in Western Europe, is the section that shows
a distinct stratigraphical succession, with fully developed Upper
Sulurian rocks below, and fully-developed Carboniferous Limestone
above, and a series of Devonian slates and limestones and their
peculiar fossils between? Thereis no such section ; but if such had
been the order of nature, surely we should by this time have some-
where found a section to prove it.

But the case is even simpler and stronger than that, for not
only is there no section exposing the three formations in regular
succession, but I have yet to learn the place where a fully-deve-.

368 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

loped set of the marine Devonian rocks are covered by anything
like a complete series of Carboniferous Limestone. Where the two
things are present, as near Cork, they are neither of them so com-
plete as in adjacent areas where only one is found.

But by the hypothesis which I now propose, the place of these
marine Devonian beds will be fixed stratigraphically between the top
of the Old Red Sandstone and the base of the Coal-measures, in
North Devon as in Ireland.

I cannot yet speak from personal Paninatien of South Devon,
but, from the descriptions of Sedgwick and Murchison and others,
it appears to have a more complicated structure than North Devon.
The occurrence of red sandstones above the Plymouth limestones
(Trans. Geol. Soc. vol. v. p. 657) might at first appear to place those
limestones below the Old Red Sandstone. On this point I may,
by way of caution, refer to the previous remarks at p. 323, that it
is not every group of red sandstones, with some beds even of Car-
boniferous Limestone immediately over them, that is entitled to
be called Old Red Sandstone. We have in Ireland beds of red
and yellow sandstones and conglomerates in the Carboniferous Lime-
stone; there is no reason, therefore, why similar beds may not oc-
cur 7 the Devonian beds of Devonshire. In neither case should
these red sandstones be identified with the Old Red Sandstone
proper.

The true Old Red Sandstone is the conformable base of the great
Carboniferous series, and contains no marine fossils; the Devonian
beds proper (those containing marine fossils) lie above it, side by
side with the Carboniferous Limestone, both being directly covered
by the Coal-measures.

The difference in the fossils of the Carboniferous Limestone and
the Devonian beds must then be held to be the result of space
rather than of time, and to mark the influence of nature of bottom
and difference of province, rather than of chronological periods.

This difference will be somewhat analogous to that observable in
the case of the Upper Silurian rocks of North Wales and of Siluria
proper. The Wenlock rocks of Denbighshire abound with impres-
sions of the various species of Theca (Q. J. G.S8. vol. 1. pl. 13),
so that they might well be called Theca flagstones; but this fossil
is either entirely absent from the Wenlock rocks of Siluria proper *, or
very rare in them, while the common Wenlock fossils are rare in
Denbighshire.

The difference noted by M. Barrande between the Trilobites in
the contemporaneous Silurian beds of Bohemia and Scandinavia will
occur to every geologist as a still more striking instance.

- The influence of geographical distribution, which is so obvious on
the existing species of animals and plants, has hardly yet, I think,
been sufficiently allowed for by paleontologists. As we trace forma-
tions through different countries, we must hold ourselves prepared
to find the same species in beds not strictly contemporaneous, and

* Theca anceps is mentioned by Mr. Salter as found near Eastnor Castle,
Malvern Hills. Mems. Geol. Surv. vol. ii. p. 255. .

1866.] | jJUKES—OLD RED SANDSTONE AND DEVONIAN, 369

different species in beds which are so—and this sometimes within
very narrow geographical limits.

13. General conclusion.—I would, then, beg leave to suggest, in the
first place, that the identification of the Old Red Sandstone proper
with the Devonian beds was an over-hasty conclusion, and that,
till the question be finally settled, it would be well to discontinue
the use of the term Devonian for all beds which are, or are sup-
posed to be, really Old Red Sandstone. One source of confusion
would thus be avoided. The term “ Devonian” would then be
confined to beds containing those species and genera of Brachiopoda
and other marine fossils which are commonly understood when we
speak of Devonian fossils. The Old Red Sandstone certainly does
not contain any of these fossils. The plants and the Anodonta
which it does contain seem to point to a freshwater origin for it,
or at all events the neighbourhood of land.

The Devonian beds, when the Old Red Sandstone is detached
from them, will still be sufficiently extensive and important. The
peculiar genera and species belonging to them seem to have a very
wide range over the world in general, quite as wide perhaps as the
genera and species peculiar to the Carboniferous Limestone.

I believe, however, that it will ultimately be found that the
genera and species which have the widest range of all, are those
which are common to the Devonian beds and the Carboniferous
Limestone.

It may doubtless be thought a bold, not to say audacious, spe-
culation, but it occurs to me to ask whether we ought not rather
to look upon the Devonian beds as the most general type of those
which intervene between the Coal-measures and the Old Red Sand-
stone, and regard the Carboniferous Limestone of the British Islands
and Belgium as a local and exceptional peculiarity: It seems to
me that good reasons might be urged for such a classification.
It would be represented in a condensed form in the subjoined
diagram.

Fig. 18.

Lower Coal-measures, with Posidonomya, Aviculopecten, Lunulacardium,
Goniatites, Orthoceras, Celacanthoid Fish, &c. :

Carboniferous
Limestone. .

Devonian beds, or Carboniferous slate with Cypridinenschiefer, Strin-
gocephalus-, and Calceola-limestones, Spiriferensandstein, Marwood and
' os oe Coomhola sandstones, &e. &c.
eee ee Bea ak de a el a) Be ete Ciel fi, iia
Old Red Sandstone, with Adiantites or Cyclopteris and other Ferns, Knorria,

Sagenaria, Cyclostigma and other plants, Anodonta, and fish of the genera
Coccosteus, Glyptolemus, Phaneropleuron, Glyptopomus, &e. &e. &e.

[SiS ee EE a ee Ea |

370 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 7,

_ Where the Old Red Sandstone is absent, the Devonian beds may
perhaps repose conformably on the Upper Silurian, or unconformably
either on that or some lower formation.

IV. APPENDIX.

My colleague, Mr. R. Etheridge, has at my request drawn up a
complete catalogue of all the British fossils of the Devonian and
Old Red Sandstone formations, so far as they are at present known,
with all the recent improvements in their nomenclature introduced
by Mr. Davidson and others. He has also shown their distribu-
tion, in parallel columns, in the several districts of Cornwall, South
Devon, and North Devon, subdividing the beds which occur in
those districts into the ordinarily received groups. He has also
subdivided the Old Red Sandstone into Upper, Middle, and Lower,
according to the prevailing ideas as to the grouping of those beds.
He has added columns for Ireland, one showing the fossils which
occur only in the Coomhola Grits, the other, including these, in a
list which shows the whole fossils hitherto recorded from any part
of the Carboniferous Slate of Ireland. He has then shown, in
farther columns, the species which also occur in the Carboniferous
formations in other parts of the British Islands, taking the com-
monly received subdivisions of that formation; and, lastly, has
given columns which mark the occurrence of any of the species
enumerated in the Rhenish Provinces, in Belgium, and in France.
Mr. Etheridge, in drawing up this list, has carefully confined him-
self to the recording of facts from the best authorities, irrespectively
of all hypotheses as to the classification of the beds.

He then gives a Table, in which the numbers of species are com-

bined under their respective biological headings. From this it ap-
pears that the whole number of species is 529, of which, however,
112 are fish that occur only in the Old Red Sandstone. If we omit
these from the total, as not affording any element of comparison, and
also omit the 12 species of plants, in order to confine the com-
parison to undoubtedly marine organisms, we have a total of 405 of
such organisms. Of these one only (Serpula advena) has been
found in the Old Red Sandstone. If we omit this, and also the
freshwater Anodon of the Old Red Sandstone, it leaves 403, or in
round numbers, 400 species of marine organisms found in the ma-
rine Devonian beds for comparison with fossils of the same class in
other formations. Of these 400 species, 13 only, chiefly Corals, are
said to occur in any Silurian rocks, while 92, or nearly a quarter of
the whole, occur in the undoubted Carboniferous rocks of other
parts of the British Islands.
_ It also appears from the Table that the paleontological differences
between different areas of the Devonian beds are at least as great, if
not greater, than those observable between the Devonian and the
Carboniferous Limestone series.

It is also to be recollected that the amount of difference apparent
on the comparison of lists of species, is to a certain extent delusive,

1866. ] JUKES—OLD RED SANDSTONE AND DEVONIAN. O71

since a species founded on a single specimen, or a few rarely occur-
ring specimens, counts as much in this comparison as a species of
' which specimens occur everywhere in the greatest profusion.

The abundance of individuals must be an element of importance
towards the establishment of a species, as enabling the paleontolo-
gist to include all its varieties; but, even in two equally distinct
species, it appears to me that richness in individuals and eatent of
diffusion ought to be taken into account by the geologist, when esti-
mating their potency in chronological significance.

Tables of percentage in which abundance and diffusion of species
are not taken into account are really of no great value. I strongly
suspect that the ninety-two carboniferous species mentioned above
include those which are at the same time most abundant and most
widely diffused in both groups of rock, while the rare and doubtful
species will be found entirely among the remainder. Some of the
latter, too, will eventually be decided to be mere varieties of the
former, and will therefore be not only erased from the one list, but
added to the other.

372

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From January 1st to March 31st, 1866.

I. TRANSACTIONS AND JOURNALS.

Presented by the respective Societies and Editors.

American Journal of Science. Second Series. Vol. xl. No. 120.
November 1865.

A. Winchell.—Indications of a Northward Transportation of Drift
Materials in the Lower Peninsula of Michigan, 331.

History of Eozoén Canadense, 344 (plate).

Notices of Earthquakes, 362.

A. A, Julien.—Metabrushite, Zeugite, Ornithite, and other minerals
of the Key of Sombrero, 367.

W. P. Blake.—Iron-regions of Arizona, 388.

G. A. Shufeldt, jun.—Oil-well boring at Chicago, 388. .

L. Agassiz.— Drift in Brazil, and Decomposed Rocks under the Drift,
389,

Mining Statistics of Great Britain for 1864, 390,

Cretaceous Reptiles of the United States, 391.

J. D, Dana.—Discovery of Rhizopods in the Azoic Rocks, 391.

R. E. Owen and E. T. Cox.—Mines of New Mexico, 391.

J. Barrande’s ‘ Défense des Colonies,’ Part iii., noticed, 392.

New Dinosaurian from the Isle of Wight, 392.

—. Second Series, Vol. xli. No. 121. January 1866.

W. B. Dwight.—Boulder- and Glacial Scratches at Englewood, 10.

—. Subsidence of land at Coxsackie, 12.

A. S. Packard, jun.—Drift-phenomena of Labrador and the Atlantic
coast southward, 30.

T. A. Conrad.—New group of Eocene Shells, 96.

Knop.—Pachnolite, a new mineral, 119.

F. A. Genth.—Chrysolite with Chromic Iron in Pennsylvania, 120,

W. P. Blake.—Crystallized Gold in California, 120.

J. P. Lesley—Asphalt vein in Wood Co., Western Virginia, 4.

DONATIONS, Sie

American Journal of Science. Second Series. Vol. xli. No. 121
(continued).

A. Winchell.—Descriptions of Fossils of the Marshall Group of
Michigan, 120.

H. A. Green.—Fossiliferous localities in Livingston and Genesee
Counties, 121. ae

F, B. Meek and A. H. Worthen.—New types of organic remains from
the Coal-measures of Illinois, 123.

_ Remarks on the genus Tavxocrinus, 124.

J. P. Lesley.—Geological position of oil-wells, 139.

Malta cavern, 140.

Anthropological Review. Vol. iv. No.12. January 1866.

Art-Union of London. Report of Council for 1865, with List of
Members. |

Assurance Magazine. Vol. xii. No. 62, January 1866.
——, General Index to the first ten Volumes. 1864,

Atheneum Journal. Nos. 1993-2005. January to March 1866,
Notices of Meetings of Scientific Societies, &c.
J. J. Lake.—Flint Age, 102.
G. Greenwood.—Rain and Rivers, 246,
H. James.—Theory of Geological Phenomena, 430.

Basel. Verhandlungen der naturforschenden Gesellschaft. Vol. iv.
Heft 2. 1866.

P. Merian.—Ueber die Pflanzenabdriicke in dem Uebergangsgebirge
von Badenweiler, Grossherzogthum Baden, 254.

L. Riitimeyer.—Beitriige zu einer paleeontologischen Geschichte der
Wiederkauer, zunachst an Linné’s Genus Bos, 299.

A. Miiller.—Ueber die Ivystallinischen Gesteine der Umgebungen
des Maderanerthales, 359,

Berwickshire Naturalists’ Club. Proceedings. Vol.v. No.3. 1865,
_ From George Tate, Esq., F.G.S.
G. Tate.—Records of Glaciated Rocks in the Hastern Borders, 236.
Briinn. Verhandlungen des naturforschenden Vereines. Vol. iii.
1864.

C. Schwippel.—Das Rossitz-Oslawaner Steinkohlengebiet, 3 (plate).

J. Sapetza.—Geognostische und mineralogische Notizen aus der
Umgebung von Neutitschein, 17.

A. Oborny.—Skizzen als Beitrige zu den geognostischen und mine-
ralogischen Verhaltnissen des mahrischen Gesenkes, 31.

Calcutta. Asiatic Society of Bengal. Journal. New Series. Part I.
No. 3. 1865.

——, Part II. No.3. 1865.

Canadian Journal of Science and Art. New Series. Vol.x. No. 60.
November 1865,

K, J. Chapman, Minerals from Lake Superior, 406,

——ee

374 DONATIONS.

Canadian Naturalist and Geologist. New Series. Vol.ii. No. 5.
October 1865.

R. I. Murchison.—Address to Geological Section of British Asso-
ciation at Birmingham, 1865, 321.

Chemical Society. Journal. Second Series. Vol. iii. No. 36.
December 1865.

——. ——. ——.. Vol.iv. Nos. 37&38. January and Fenny
1866.

Colliery Guardian. Vol. xi. Nos. 262-274. January to March 1866.

Notices of Meetings of Scientific Societies, &e.

Coal in Africa, 43.

Geology of Australia, 43.

Geological Survey of India, 103.

Coal in Japan, 152.

Coal-supply of Europe and America, 190, 208.

C. Hardwick.—Geology in its relation to Archeology, 242.

Geological Magazine. Vol.iii. Nos.1-3. January to March 1866.

Geological Progress. No. 3., 1.

R. Etheridge.— Discovery of several new Labyrinthodont Reptiles in
the Coal-measures of Ireland, 4.

E. Hull.—Raised Beach of Cantyre, 5.

H. Woodward.—New Crustacean (ger Marderi, H. W.) from the
Lias of Lyme Regis, Dorsetshire, 10 (plate).

C. J. A. Meyer.—Correlation of the Cretaceous Rocks of the South-
east and West of England, 13 (plate).

Quarterly Journal of the Geological Society, noticed, 29,

Barrande’s ‘Systéme Silurien du centre de la Bohéme,’ lve Partie:
“Recherches Paléontologiques.” Vol. ii. “ Céphalopodes: 1? Série,”
noticed, 32.

Agassiz’s “Seaside Studies in Natural History,’ noticed, 36.

E. W. Binney.—So-called Lower New Red Sandstones of Central
Yorkshire, 49.

R. Owen.—New Sauroid Fish from the Kimmeridge Clay, 55 (plate).

S. V. Wood, jun.—Structure of the Thames Valley, 57, 99.

D. Mackintosh.—Sea y. Rain and Frost, 63.

Lartet and Christy’s ‘ Reliquiee Aquitanice,’ Part I., noticed, 76.

Cotta’s ‘Geology and History,’ noticed, 77.

Hittel’s ‘ Resources of Canada,’ noticed, 78.

J. Phillips.—Oxford Fossils, No. 2 OE ‘(plate).

R. Owen.—New Genus of Sauroid Fish from the Resear Clay,
107 (2 plates).

E. C. H. Day.—Ancient Beach and Submerged Forest near Wissant,
109 (plate).

Raised Beach and Cave at Weston-super-Mare, 115.

Petroleum and Oilfields in their Geological Aspect, 120.

E. W. Binneys ‘ Fossil Coal-plants showing structure,’ noticed, 126.

A. von Koenen’s ‘Fauna of the Lower Oligocene Tertiary. Beds of.
Helmstidt,’ noticed, 127.

Abstracts of British and F oreign Memoirs, 19, 71, 119.

Reports and Proceedings of moans 22, 78, 128,

Correspondence, 46, 84, 137.

Miscellaneous, 48, 94, 143,

DONATIONS, 375

Geological and Natural History Repertory. Vol. 1. Nos. 9-11.
January to March 1866.
‘Frost and Fire,’ noticed, 198.
S. J. Mackie.—Natural Fractures of Flints, 205.
“Notes and Queries, 119, 214.
Biographical Notices, 119, 222, 234.
Proceedings of Societies, 217, 225,

Giessen. Ambtlicher Bericht iiber die neun und dreissigste Versamm-
lung deutscher Naturforscher und Aerzte. 1865.
Schmidt.—Ueber Meteoriten, 104.
Ludwig.—Ueber die Thiatigkeit des mapithciaiaghon geologischen
Vereins, 107.
Ueber die Ablagerungsformen der Braunkohle zu Dornheim,
108.

Rose.—Die Meteoriten, 111 (plate).

V. Diicker.—Ueber die Gebirgsformationen der Schweiz, 122.

V. Klipstein.—Die Eisensteinlagerstiitten am Eggebirge bei Pr.-
Oldendorf, 131.

——. Ueber die Entstehung phosphorhaltiger Mineralien, 135..

Household Magazine. Vol.i. No.1. January 1866.

Institution of Civil Engineers. Abstracts of Proceedings. Nos. 4
5,9 &11. 1865-66.

List of Members. 1866.

Intellectual Observer. Vol. vii. No. 48. January 1866.

D. T. Ansted.—Mud-volcanoes and Salt-lakes in the Crimea, 409.

J. Jones.—Our Future Coal-fields, 435.

A. 8. Herschel.—Hot Springs and other Natural Features of the
Pyrenees, 439.

——. Vol.ix. Nos.49 & 50. February and March 1866.

Fossil Lizard in Copal, 80.

B. H. Woodward.—Rambles in Cornwall for Minerals and Ferns, a

D. T. Ansted.— Winter visit to Mount Etna, 125,

Pre-historic Man in France, 132.
H. J. Slack.—Comparative Geology of the Earth and Moon, 185.

Lausanne. Bulletin de la Société Vaudoise des Sciences Naturelles.
vol, vii. No. 53, 1865.
J. Delaharpe.—Roc poli et strié de Chillon. Terrasses diluviennes
du bassin du Léman, 341.
E. Renevier.—Rapport pour l’année 1864, du Conservateur des col-
lections géologiques et minéralogiques du Musée cantonal, 346,

Linnean Society. Journal. Vol.ix. No. 36. 1865.

London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xxxi. Nos. 206-208. January to March 1866.
From Dr. W. Francis, F.G.S. 7
_ J. Croll._—Excentricity of the Earth’s Orbit, 26.

R.-Edmonds.—Earthquakes and extraordinary agitations of the sea,
45.

A. Sedgwick.—Geology of Dent, 79.

G. F. Browne.—Ice-caves, 82,

376 DONATIONS.

London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xxxi. Nos. 206-208 (continued). .

P. M. Duncan.—Impressions of Selenite in the Woolwich Beds and
London Clay, 155.

O. Fisher.—Relation of the Chillesford Beds to the Norwich Crag, 156.

E. B. Tawny.— Western limit of the Rhetic Beds in South Wales, 157.

Je Raat cr of Lower Lias and Rheetic Beds near Wells,
157.

J. W. Dawson.—Conditions of the Deposition of Coal, 158.

W. King and T. H. Rowney.—Origin and Microscopic Structure of
the so-called Eozoon Serpentine, 159.

W. B. Carpenter.—Supplemental Notes on the Structure and Affini-
ties of Hozoon Canadense, 159.

R. A. C. Godwin-Austen.—Notes on Belgian Geology, 237,

How.—Mineralogy of Nova Scotia, 165.

Pratt.—Level of the Sea during the Glacial Epoch in the Northern
Hemisphere, 172.

KE. J. Chapman.—Minerals from Lake Superior, 176.

D, D. Heath.—Secular Local Changes in the Sea-level, 201.

London Review. Vol. xu. Nos. 288-300. January to March 1866.

Notices of Meetings of Scientific Societies, &c.
B. Gastaldi’s ‘Lake Habitations and Prehistoric Remains in the
Turbaries and Marl-beds of Northern and Central Italy,’ noticed,

The Scientific Year.—Geology, 48; Mineralogy, Metallurgy, and
Mining, 50,

Longman’s Notes on Books. Vol. ii. No. 44. February 28, 1866.
Magazine of Anthropology. Vol.i. No.1. January 1866.

Manchester Geological Society. Transactions. Vol. vy. No. 12.
1865-66.
J. Aitken.—Union of the Gannester and Higher Foot Coal-mines at
Bacup, 185.

Milan. Atti della Soctetd Italiana di Scienze Naturales yolaeam
Fase. 2. 1865. -

Omboni—Relazione sulle condizioni geologiche delle ferrovie pro-
gettate per arrivare a Coira passando per lo Spluga, 97,

Neuchatel. Bulletin de la Société des Sciences Naturelles, Tome vii.
i Cahier, eGo. 4
M. de Rougemont.—Epoques antédiluvienne et celtique du Poitou, 87.

Offenbach am Main. Sechster Bericht des Vereins fiir Naturkunde.
1865.

Paris. Annales des Mines. Sixicéme Série. Vol.viu. Livr.4. 1865.

Bulletin de la Société Géologique de France. Deuxicme
Série. Vol. xxii. f. 27-36. May to June 1865.
Virlet.—Sur le minerai de fer alumineux oolithique de Mouriés (ou
des Baux), 418.
L. Lartet.—Sur la formation du bassin de la mer Morte et sur ses
changements de niveau, 420 (plate),

DONATIONS. OUF

Paris. Bulletin de la Socicté Géologique de France. Deuxiéme
Série. Vol. xxi. f. 27-36 (continued).

Virlet.—Sur les salures différentes de certains lacs du Mexique, 464.

F. Garrigou.—Apereu géologique sur le bassin de l’Ariége, 476 (plate).

De Chasteigner.—Sur les silex taillés du bassin de la Creuse, 513.

Y. de Moeller.—Sur la géologie de diverses parties de la Russie
d’Europe, 517. ;

Eid. de Verneuil.—Sur une dent d’Eléphant trouvée dans le diluyium
de la riviére Aniene, pres de Rome, 519.

. Sur quelques ossements fossiles recueillis dans le diluvium du
Tibre, prés de Rome, 521.

Bleicher.—Sur une petite dent d’Elephas antiqaus, 522.

——. Sur les dépots diluviens de la campagne romaine, 524.

J. Marcou.—Addition a sa note du 6 mars dernier, p. 290, 529.

Irgens et Hiortdahl.—Sur quelques roches éruptives de la céte ouest
de la Norvége, 530.

L. Lartet.—Sur la découverte de silex taillés en Syrie et sur lage
des terrains de la chaine du Liban, 537 (plate).

Edm. Pellat.—-Sur la zone a Avicula contorta et le bone-bed au sud-
est d’Autun, dans les environs de Couches-les-Mines, 546.

Th. Ebray.—Sur une conséquence de la verticalité de certains filons,

565.

. Comptes Rendus des Séances de ?Académie des Sciences.
Table des Matiéres du tome lx. January to June 1865.

Jacquot.—Sur le gisement des sources minérales du département du
Gers, et sur les relations qui les rattachent au systéme des Pyré-

nées, 967,
Sandras.—Etudes sur les eaux minérales phosphatées ferrugineuses,

1160.

Gervais.—Sur le Mesosawrus tenwidens, reptile dont les restes fossiles
ont été trouvés dans l’Afrique australe, 950.

Bianconi.—Recherches sur les os de l’Epiornis maximus, 179.

E. de Beaumont.—Sur une Note de M. Sismonda sur un gneiss avec
empreinte d’ Eguesetum, 492.

Marés.—Sur la constitution du sud de la province d’Alger, 1039.

Mallard.—Sur une roche magnétique trouvée au Puy Chopine, Puy-
de-Déme, 1068.

Pissis.—Sur les volcans et les terrains récents du Chili, 1095.

Liais.—Sur quelques faits géologiques observés dans le bassin du Rio
de las Velhas, un des principaux affluents du San Francisco, 1200.

Pisani.—Sur la calicine, nouvelle espéce minérale trouvée 4 Chypis
en Valais.—Sur la limonite pisolitique d’Iwaro, Hongrie, 918.

Meillet.—Sur les ateliers d’instruments en silex des environs de
Chatellerault, 35.

G. de Mortillet.—Sur les haches en Néphrite de la Suisse, 83.

Lioy.—Sur les habitants des cavernes et des cités lacustres, 85.

Husson.—Sur des portions de deux machoires humaines provenant
de cavernes 4 ossements, 111.

EK. Robert.—Observations critiques sur lage de pierre, 664.

Mortillet.—Sur les silex taillés du Grand-Pressigny, 745.

Husson.—Alluvions des environs de Toul pour rapport a l’ancienneté
de homme, 784. Pods

Dupont.—Sur les terrains quaternaires de la Belgique, 863.

Longobardo.—Sur une nouvelle éruption de l’Etna, 364.

Fouqué.—Sur l’éruption de Etna du 31 janvier, 1865, 548.

VOL, XXII,—-PART 1, 2D

378 DONATIONS.

Philadelphia. American Philosophical Society. Proceedings. Vol. x.
No. 74. 1865.
J. P. Lesley.—Oil-Well Borings, 187.

——., Transactions. New Series. Vol. xiii. Part 2. 1865.

Photographic Journal. Vol. x. Nos. 165-167. January to March
1866.

Plymouth Institution. Annual Report. 1864-65.

W. Pengelly.—Red Sandstones, Conglomerates, and Marls of Devon-
shire, 13.

Quarterly Journal of Microscopical Science. New Series. Vol. xiv. —
No. 21. January 1865.

Quarterly Journal of Science. Vol. iii. No.1. January 1866.

A. C. Ramsay.—Recurrence of Species in Geological Formations, 33.
Origin and Antiquity of Man, 64.
Chronicles of Science, 77.

Reader. Vol. vu. Nos. 158-170. January to March 1866.

Notices of Meetings of Scientific Societies, &c.

Belgian Bone Caves, 42.

The Glacial Submergence, 44, 208.

EK. Lartet and H. Christy’s ‘ Reliquize Aquitanicz,’ noticed, 69.

G. H. Kinahan.—Castlecomer Fossils, 70.

8. V. Wood, jun.—The Glacial Submergence, 98.

O. Fisher.—The Glacial Submergence, 155. ;

S. Laing’s ‘ Prehistoric Remains of Caithness,’ noticed, 180.

N. Whitley.— Flint Finds,” 183.

D. Page’s ‘Geology for General Readers,’ noticed, 328.

J. Nicol’s ‘Geology and Scenery of the North of Scotland,’ noticed,
328.

Physical Aspects of Palestine, 231, 257, 280, 304, 328.

S. V. Wood, jun.—Geological Maps, 331.

Regensburg. Correspondenz-Blatt des zoologisch-mineralogischen
Vereines. Nos. 1&2. January 1866.

A. F. Besnard.—Die Mineralogie in ihren neuesten Entdeckungen
und. Fortschritten, 7.

Royal College of Physicians. List of Members, Extra-Licentiates,
and Licentiates. 1866.

Royal College of Surgeons of England. Calendar. 1865.

Royal Geographical Society. Proceedings. Vol. x. Nos. 1 & 2.
1866.

Royal Geological Society of Ireland. Journal. Vol.i. Partl. 1865.

M. H. Close.—Glaciation of the Rocks in the Neighbourhood of
Dublin, 3 (plate).

J. B. Doyle.—Notes on the Occurrence of a well-marked Specimen of
Knorria in the Lower Carboniferous Limestone Series of Kildare,
13.

Hf. B. 8. Montgomery.—New Locality of Granite in Limestone near
Rathfarnham, 15,

DONATIONS, 379

Royal Geological Society of Ireland. Journal. Vol. i. Part 1 (con-
tonued).

A. Macalister.—Specimen of Ulodendron, found at Hurlet, Renfrew-
shire, 16.

M. H. Ormsby.—Polished and striated surface in the Limestone of
Ross Hill, Galway, 18.

W. Harte. — Physical features of the county of Donegal, 21 (plate).

S. Haughton.—Geological Notes on some of the Islands of the West
of Scotland, 28.

F, J. Foot.—Recent Erratic Block, 32.

J. Kelly.— Remarks on the doctrine of Characteristic Fossils, 34.

W. L. Lindsay.—Geology of the New Zealand Gold-fields, 49.

J. Wright.—Description of a new Palechinus, 62.

W. H. Baily.—Structure of Palechinus, 63 (2 plates).

W. Harte.—New Hchinoderm from the Yellow DS idetena of Donegal,
67.

Royal Horticultural Society. copes pea Vol.v. No.9. December
1865.

——. ——. NewSeries. Vol.i. No.1. January 1866.
——. Journal. New Series. Vol.i. Part 1. January 1866.

Royal Society. Proceedings. Vol. xiv. Nos. 79-61. 1866.
W. H. Miller.—Graphitoidal Silicon and Graphitoidal Boron, 11.

Society of Arts. Journal. Vol. xiv. Nos. 685-697. January to
March 1866.
Notices of Meetings of Scientific Societies, &c.
Geology of Australia, 130.
American Mineral Resources, 349.

Stockholm. Kongliga Svenska Vetenskaps-Akademiens Handlingar.
Ny Foljd. Femte Bandet. Forsta Hiftet. 1863.

——. Ofversigt af Kongl. ee eee Forhandlingar.
Tjugondeforsta Argfingen. 1865.

Nordenski6ld.—N ya forvarf vid mineral-kabinettet, 74, 415.
Paykull.—Mineralogiska iakttagelser, 207.

Turin. Bullettino Trimestrale del Club Alpino. No. 1. August
) 1865, 7 |

Vienna. Jahrbuch der k.-k. geologischen Reichsanstalt. Vol. xy.
Nos. 2&3. April to September 1865.

H. Wolf.—Ueber die Gliederung der Kreideformation in Bohmen, 183.
I’. v. Hochstetter.—Ueber das Vorkommen von Erdol (Petroleum)
und Erdwachs im Sandecer Kreise in Westgalizien, 199.
A. Madelung.—Ueber das Alter der Teschenite, 208.
F. Posepny.—Ueber ein Jura-Vorkommen in Ost-Galizien, 218.
F.. Ambroz.—Geologische Studien aus der Umgebung von Padert, 215.
Simettinger.—Die Stubinggraben, 248.
D. Stur.—Vorkommen ober-silurischer Petrefacte am Erzberg und in
dessen Umgebung bei Hisenerz in Steiermark, 267.
Fossilien aus den neogenen Ablagerungen von Holubica bei
Pieniaky sitidlich yon Brody im éstlichen Galizien, a
2D

3880 DONATIONS.

Vienna. Jahrbuch der k.-k. geologischen Reichsanstalt. Yol. xv.
Nos. 2 & 3 (continwed).

F. Kaufmann.—Ueber den Dopplerit von Obbiirgen und tiber das Ver-
hiltniss des Dopplerits zu Torf und mineralischen Kohlen, nebst
Bemerkungen tiber kiinstliche pechkohlenartige Substanzen, 283.

G. Stache.—Bericht iiber die geologischen Autnahmen im Gebiete
des oberen Neutra-Flusse und der koniglichen Bergstadt Kremnitz
im Sommer 1864, 297. jt

F. Daubrawa.—Die geologischen Verhiltnisse des Bezirkes Mahrisch-
Neustadt, zum Theil auch jener von Miglitz Hohenstadt, Schon-

berg, Romerstadt, Littau, und Sternberg, 320.

K. M. Paul.—Das linke Waagufer zwischen Sillein, Bistritz, und dem
Zilinkaflusse im Trentschiner Comitate, 336.

F, Posepny.—Das Vorkommen und die Gewinnung von Petroleum
im Sanoker und Samborr Kreise Galiziens, 351.

A. Patera.—Das k.-k. hiittenmannisch-chemische Laboratorium in
Wien, 359.

K. von Hauer.—Der Salinenbetrieb an den Sudwerken zu Hallein und
Hall in chemischer Bezichung, 369.

P. O. Werdmiuller.—Hohe1.messung einiger Wasserfalle, 391.

Verhandlungen der k.-k. geologischen Reichsanstalt 1865.

Kaiserliche Akademie der Wissenschaften in Wien. Anzeiger.
Jahre, 1865.-4 Nos. 17-19.
M. Hornes.—Geognostische Karte des ehemaligen Gebietes yon
Krakau, 198.
Ei. Suess.—Monoeraphie der Echinodermen des Hifler Kalkes, 199.
C. R. v. Ettingshausen.—Vie fossile Flora des Tertiarbeckens yon
Bilin, 200. eae,
I. v. Hauer.—Ueber eine neue Cephalopoden-Sippe Choristoceras
aus den Kossener-Schichten, 207.
G. Tschermak.— Untersuchung eines Feldspathgesteines, 209.

sseqiihast sisi taheeadeee, kNogeia7e

F, vy. Hochstetter—Ueber das Vorkommen von Hozodn im krystalli-
nischen Kalke von Krummau im stidlichen Bohmen, 3.

G. Tschermak.—Untersuchung eines neuen Minerales yon Orawieza
im Banat, 31.

A. HE. Reuss.—Ueber die Bryozoen, Anthozoen und Spongiarien des
braunen Jura von Balin bei Krakau, 35,

ihe Laube.—Die Bivalven des braunen Jura yon Balin bei Krakau,

IT, PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. Third Series. Vol. xvii.
Nos. 97-99. January to March 1866.

S. Haughton’s ‘Manual of Geology,’ noticed, 65.

Peters.—Fossil Lizard in Copal, 78.

IL. Seeley. —On Torynocrinus and other new and little-known Fossils
from the Upper Greensand of Hunstanton, commonly called the
Hunstanton Red Rock, 173.

W. Kine.—Tubulation of the Valves of Rhynchopora Geimitziana, De
Verneuil, 230,

DONATIONS, 381

Leonhard und Geinitz’s Neues J ahrbuch fiir Mineralogie, Geologie,
und Paliontologie. Jahrgang 1865. Heft 7.

Schafhautl.—Die Nummuliten-fiihrenden Schichten des Kressen-
berges, 769.

. Der weisse Jura im Wettersteingebirgstock und der Lias im
Hochfelln der bayerischen Alpen, 789 (plate).

Credner.—Geognostische Reiseskizzen aus New Brunswick in Nord-
Amerika, 803.

Letters ; Notices of Books, Minerals, Geology, and Fossils.

——. J ahrgang. 1866. Heft 1.

T. Scheerer.—Beitrage zur Erklarung der Dolomit-Bildung mit
besonderer Hinsicht auf die Dolomite Sudtyrols, 1.

I’. Sandberger.—Die Stellung der Raibler Schichten in dem frankis-
chen und schwabischen Keuper, 34.

P. Groth.—Ueber den Titanit im Syenit des Plauen’schen Grundes,
45.

EK. Poppe.—Ueber fossile Friichte aus den Braunkohlen-Lagern der
Oberlausitz, 52 (plate).

R. Ludwig. —Die Mainzer und Hessische Tertiar-Formation, 59.

Letters; Notices of Books, Minerals, Geology, and Fossils.

L’Institut. 1 Section. 33° Année. . Nos. 1665-167
——. - 2° Section. -30° Année. Nos. 359-361.

Paleontographica: herausgegeben von Hermann von Mayer. Vol.
xiv. Lief. 4. November 1865.

R. Ludwig.—Corallen aus paliolithischen Formationen, 183 (14
plates).

———+ ———, _ Vol. xv. Lief. 1. November 1865:

H. von Meyer.—Ueber die fossilen Reste von Wirbelthieren, welche
die Schlagintweit von ihren Reisen in Indien und Hoch-Asien
mitgebracht haben, | (8 plates).

Zu Chelydra Dechent aus der Braunkohle des Siebengebirges,

4] ‘(plate).

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.

bik! H. Beitrage zur geologischen Kenntniss der oo
in den kaukasischen Liindern. 1865.

Anon. ‘Coal Mines.° 1858.° Fron W. Whitaker, Bags F.GS.

Glaciers and their phenomena. 1859. From W. Whitaker,
Esq., F.GS.

Soentn Scientiarum. Being some account of te origin and
objects of the Victoria oe or Philosophical Society of Great
Britain, 1865.

382 DONATIONS,

Benecke, EH. W. Geognostisch-paliontologische Beitrige. Vol. i.
Heft 1. Ueber Trias und Jura in den Siidalpen. 1866.

Binney, E.W. A Description of some Fossil Plants, showing struc-
ture, found in the Lower Coal-seams of Lancashire and Yorkshire.
1865.

. A few remarks on Mr. Hull’s Additional Observations on fhe
Drift Deposits in the neighbourhood of Manchester. 1865,

Further Observations on the Permian and in ‘assie Strata of
- TLaneashire. 1865.

On some of the objects of the Manchester Geological Society,
and the best means of attaining them. 1865.

Bland, T. Note on the internal structure of Megaspira. 1866.

Notes on certain Terrestrial Mollusca, with Descriptions of
New Species. 1865.

Remarks on the origin and distribution of the operculated
land-shells which inhabit the continent of America and the West
Indies, with a Catalogue of the American species. 1866.

Brown, R., The Miscellaneous Botanical Works of. Vol. i., con-
- taining, I. Geographico-Botanical, and II. Structural and Physio-
logical Memoirs. 1866. From the Ray Society.

California. Geological Survey. Report of Progress and Synopsis of
the Fieldwork, 1860- 64. Geology. Vol.1. 1865. From Prof.
J. D. Whitney. :

Catalogue. Catalogue of the Organic Remains belonging to the
Echinodermata, in the Museum of the Geological Survey of India,
Calcutta. 1865. From Dr. T. Oldham, F.GS.

—. Official catalogue of the Italian Contributions to the Dublin
International Exhibition, 1865. From W. P. Jervis, Esq., F.GS.

Christiania. Det kongelige Norske Frederiks tee Aarsbe-
retning for aaret 1863. 1865.

——. Gaver til det kgl. Norske Universitets 1 Christiania. 1863.

Gaver til det kongl. Norske Universitets Bibliothek i Chris-
tiania indkomne gjennem Universitets Secretariat 1 4de Quartal
1863. 1864.

. Index Scholarum in Universitate Regia Fredericiana cente-
simo quinto elus semestri anno MpcocLxv ab augusto mense ineunte
habendarum. 1865. From the University of Christiania.

Delesse. Recherches sur l’origine des Roches. 1865.

Deshayes, G. P. Description des animaux sans vertébres découverts
dans le bassin de Paris. Livraisons 47-50. 1865.

DONATIONS. 383

Duncan, P. M. On some Spaces, formerly occupied by Selenite, in
the Lower Eocene Clays of the London Basin; with remarks on
the Origin and Disappearance of the Mineral. 1866.

On the Fossil Corals of the West-Indian Islands. Part I.

B-1e65.

Eichwald, E. v. Einige Bemerkungen iiber die geognostischen
Karten des Europaischen Russlands. 1865.

Favre, A. Sur la structure en éventail du Mont-Blanc. 1865.

Fowler, J. Address on his election as President of the Institution.
of Civil Engineers, Session 1865-66. 1866. From the Institution
of Cwil Engineers.

Gastaldi, B. Sulla Riescavazione dei Bacini Lacustri per opera degh.
antichi ghiacciai. 1865.

Gastaldi, Cav. Intorno ad alcuni fossili della Toscana e del Pie~
monte. 1865.

Giebel. Herr vy. Koenen und die Latdorfer Conchylienfauna. 1866.

Gosse, P. H. Omphalos. (Review.) 1858. From W. Whitaker,
Esq., F.GS.

Greece. New Island in the Bay of Théra. (Extracts from “The
Times.”) 1866. From W. Whitaker, Esq., F.GS.

Giimbel, C. W. Geognostische Verhaltnisse der Pfalz. 1865.

— —, Ueber das Vorkommen unterer Triasschichten in Hochasien.

1866.

Guppy, R. J. £. On the Terrestrial and Fluviatile Mollusca of Tri-
nidad. 1866.

Kjerulf, L. T. Veiviser ved geologiske excursioner 1 Christiania
Omegn. (Met et farvetrykt kart og flere tresnit.) 1865.

Kokscharow, N. v. Materialen zur Mineralogie Russlands. 4 vols.
and plates. 1853-65.

——. Notiz iiber den Chiolith. 1864.

——. Ueber das Krystallsystem und die Winkel des Sylvanits.
1865.

——. Vorlesungen iiber Mineralogie. Vol.i. 1865.
Koninck, L. de. Résumé de la théorie chimique des types. 1865.

Lardner, D. Popular Geology. (Review.) 1857. From W.Wh-
taker, Esq., F.GS. :

Lartét, EH. Sur une lame ivoire fossile trouvée dans un giseme
ossifere du Périgord, et portant des incisions qui paraissent con-
stituer _ eproduction d’un Eléphant a longue criniere. 1865.

384 DONATIONS.

Lartét, E., and H. Christy. Reliquiz Aquitanicee; being contri-
butions ‘to the Archzolog gy and Paleontology of Périgord and the
adjoining provinces of Southe iy, Be Part I. 1865. From
the Executors of the late H. Ch#isty, Esq., F.G.S.

Laube, G.C. Die Fauna der Schichten von St. Cassian. Ein Beitrag
zur Paliontologie der alpinen Trias. Abth. 11. 1860.

Lavizzari, L. Nouveaux Phénoménes des Corps Cristallisés. 1865.

Le Hon, H. Histoire complete de !a grande éruption du Vésuve de
1631, avec la carte de toutes les laves de ce volcan depuis le
seizicme siécle jusqwaujour’hui. 1866.

Tiebig, J. von. Induction und Deduction. 1865.

Lovén, S. Om Ostersjon. 1864.

Luca, S. de. Ricerche sull’ estrazione della Mannite dalle foglie di
ulivo. 1865,

——. Ricerche sulla formazione della materia grassa ne’ frutti dell’
Olivo. _ 1862. .

—-—. Osservazione sulla estrazione della Mannite dalle foglie e da’
frutti di ulivo. 1865.

——. Analisi qualitativa di calcoli intestinali di Cavallo. 1865.

——_—. Ricerche chimiche sulle materie cristallizzate contenute nelle
foglie delle piante. 1865.

, eG. Ubaldini. Ricerche chimiche su’ Frutti del Mirto Aus-

_ trale e de’ Mirti comuni. 1865.

Maenetical and Meteorological Observations made at the Government
Observatory, Bombay, in the year 1863. 1864. rom the Secre-
tary of State for India.

Martins, C. Du Spitzberg au Sahara, étapes can naturaliste au
Spitzberg, en Laponie, en Hcosse, en Suisse, en France, en Italie,
en Orient, en Egypte, et en Algérie. 1865.

——. Sur la possibilité d’atteindre le Pole Nord. 1866.

Maw, G., and EH. J. Payne.. The French Universal Exhibition of
1867. Official and other correspondence, &c., relating to the plan
promulgated by M. Le Play, the French Commissioner-General for
the Exhibition Palace. 1866.

Memoirs of the Geological Survey of India. Vol. iv. Part 3. On the
Coal of Assam, with Geological Notes on the adjoining Districts
to the South, by H. B. Medlicott. 1865. Irom Dr. T. Oldham,
EGS:

. Vol. v. Part 1. Sections across the North-western Hima-
layas, from the Sutlej to the Indus, with descriptions of the fossils,
by F. Stoliczka. The Gypsum of Lower Spiti, with a list of
Minerals collected in the Himalayas, by F. R. Mallet. 1865.

DONATIONS. 385

Memoirs of the Geological Survey of India. Palontologia Indica.
Vol. iii. Parts 6-9. The Fossil Cephalopoda of the Cretaceous
Rocks of Southern India, by F. Stoliczka. Vol. iv. Part 1. On
vertebrate fossils from the Panchet Rocks, near Ranigunj, Bengal,
by T. H. Huxley. 1865. From Dr. T. Oldham, F.GS.

Montagna, C. de. Generazione della Terra, metodicamente esposta
con nuoyi principii di Geologia. 1865-66.

——. Intorno all’ esistenza di Resti Organizzati nelle rocce dette
azoiche ed alla doppia origine del granito. 1866.

Niigeli, C. alan: und Begriff der naturhistorischen Art.
1865.

Nicol, J. The Geology and Scenery of the North of Scotland. 1866.
Oppel, A. Paleontologische Mittheilungen.. Part IV. 1865.

Packard, A. S.,jun. Results of observations on the Drift Pheno-
mena of Labrador and the Atlantic Coast southward. 1866.

Page, D. Advanced Text-book of Geology. (Review.) 1857. Prom
W. Whitaker, Esq., F.G.S.

Page, T. Report on the proposed Pachour of Refuge, New Basin,
and Dock at Maryport, and their ee for ships of large
burthen. 1865.

Report. Annual Report of the Geological Survey of India, and of
- the Museum of Geology, Calcutta. 1864-65. From Dr. T. Old-
ham, F.GS.

Report of the Chief Commissioner of Mines for the Province
of Nova Scotia for the year 1865. 1866. From the Rev. D.
Honeyman, D.C.L., F.GS.

Rigaux, E. Notice stratigraphique sur le Bas-Boulonnais. 1865.

Sars, G.O. Norges Ferskvandskrebsdyr forste afsnit Branchiopoda.
1. Cladocera ctenopora. 1865.

Scebach, K.von. Ueber den Vulkan Izalco und den Bau der Central-
_ Amerikanischen Vulkane. 1865.

Seeley, H. Notice of opinions on the stratigraphical position of the
Red Limestone of Hunstanton. 1861.

——. On the Hunstanton Red Rock. 1864.

—-. On the Fossils of the Hunstanton Red Rock. 1864.

——. On a Section discovering the Cretaceous beds at Ely. 1865,
—. Notes on Cambridge Geology. 1862.

——. Notes on Cambridge Paleontology. 1861.

386 DONATIONS.

Seeley, H. On a new Lizard, with Ophidian affinities, from the
Lower Chalk (Saurospondylus dissimilis). 1865.

——. On the Ammonites of the Cambridge Greensand. 1865.
—. On the literature of English Pterodactyles. 1865.

——. On Plesiosaurus macropterus, a new species from the Lias of
Whitby. 1865.

——. On two new Plesiosaurs from the Lias. 1865.

‘—_——. Description of two new species of Chalk Starfishes. 1858.
——. A help to the identification of Fossil Bivalve Shells. 1864.
——. Mytilus spathulatus, a new Cretaceous species. 1864.

——. Notice of Torynocrinus and other new and little-known
fossils from the Upper Greensand of Hunstanton, commonly called
the Hunstanton Red Rock. 1866.

Sorby, H. C. On the organic origin of the so-called Crystalloids of
the Chalk. 1861.

Stanley, W. F. A descriptive treatise on Mathematical Drawing
Instruments, their construction, uses, qualities, selection, preser-
vation, and suggestions for improvement; with hints upon Draw-
ing and Colouring. 1866.

Winchell, A. Some indications of a northward transportation of
drift-materials in the Lower Peninsula of Michigan. 1865.

IV. BOOKS RECENTLY PURCHASED FOR THE LIBRARY.

Alberti, F. von. Ueberblick tiber die Trias, mit Bericksichtigung
ihres Vorkommens in den Alpen. 1864.

Archiac, A. d’. Introduction 4 lV’étude de la Paléontologie Strati-
graphique. 1864.

Baudon, A. Notice sur quelques Térébratules du Calcaire grossier,
non décrites jusqu’a ce jour. 1855.

Beitrige zur geognostischen Kenntniss des Erzgebirges. Auf Anord-
nung des konigl. Siichs. Oberbergamtes aus dem Ganguntersu-
chungsarchiv. Heft 1. 1865.

DONATIONS. 387

Blainville, de. Ostéographie; ou description iconographique comparée
du squelette et du systéme dentaire des Mammiferes récents et
fossiles, pour servir de base 4 la Zoologie et 4 la Géologie. 1839-64.

Brouillet, P. A. Epoques anté-historiques du Poitou, ou recherches
et études sur les monuments de l’Age de Pierre recueillis dans les
cayernes, le diluvium et les ateliers celtiques en plein air de cette
contrée. 1865.

California. Geological Survey. -Palzontology. Vol. i. Carbonife-
rous and Jurassic Fossils, by F.B. Meek. ‘Triassic and Cretaceous _
Fossils, by W. M. Gabb. 1864.

Paleontology. Vol.i. Section 1. Part 1. Tertiary
Invertebrate Fossils, by W. M. Gabb. 1866.

Capellini, G. Studi Stratigrafici e Paleontologici sull Infralias nelle
montagne del golfo della Spezia. 1862.

Coquand, H. Géologie et Paléontologie de la région sud de la pro-
vince de Constantine. 1862.

'——. Monographie Paléontologique de l’étage Aptien de l’Espagne.
1866,

Cotta, B. von. Rocks classified and described. <A Treatise on Litho-
logy. English edition, by P. H. Lawrence, with English, German,
aud French synonyms. 1866.

Dumortier, E. Etudes paléontologiques sur les dépdts jurassiques
du bassin du Rhéne. 1” Partie. Infra-lias, 1864.

——. Note sur quelques fossiles peu connus ou mal figurés du lias
moyen. 1857.

Duval-Jouve, J. Bélemnites des terrains crétacés inférieurs des en-
-virons de Castellane (Basses-Alpes), considérées géologiquement
et zoologiquement, avec la description de ces terrains. 1841.

Eek, H.. Ueber die Formationen des bunten Sandsteins und des
Muschelkalks in Oberschlesien und ihre Versteinerungen. 1865.

Egger, J.G. Der Jura-Kalk bei Ortenburg und seine Versteine-
rungen. 1858.

Die Foraminiferen der Miocin-Schichten bei Ortenburg in
Nieder-Bayern. 1857.

Die Ostrakoden der Miocin-Schichten bei aoe in Nie-
der-Bayern. 1858.

Ehrenberg, C.G. Microgeologie, das Erden und Felsen schaffende
Wirken des unsichtbar kleinen selbststindigen Lebens auf der Erde.
1854; Fortsetzung, 1856.

388 DONATIONS,

Engelhardt, C. Denmark in the Harly Iron Age, illustrated by
recent discoveries in the peat mosses of Slesvig. 1866.

Fiedler, H. Die fossilen Friichte der Steinkohlenformation. 1857.

Fonvielle, W. de. I’Homme fossile. Etude de philosophie zoolo-—
gique. 1865.

Forbes, EK. The Zoology of the Voyage of H.M.S. ‘ Herald,’ under
the command of Capt. H. Kellett. Vertebrata, including Fossil
Mammals, by Sir John Richardson. 1854.

Fromentel, EK. de. Catalogue raisonné des Spongitaires de Vétage
Néocomien. 1861.

——. Description des Polypiers fossiles de l’étage Neéocomien..

Gaudry, A. Animaux fossiles et Géologie de PAttique. 1865.

Geinitz, H. B., H. Fleck, und E. Hartig. Die Steinkohlen Deutsch-
land’s und anderer Linder Europa’s, ihre Natur, Lagerungsver-
hiltnisse, Verbreitung, Geschichte, Statistik und technische Ver-
wendung. 3vols. 1865. .

Gesner, A. <A practical treatise on Coal, Petroleum, and other dis-
tilled oils. 1861. .

Giebel, C. Die Fauna der Braunkohlenformation von Latdorf bei
Bernburg. 1864.

Gomes, B. A. Flora fossil do terreno Carbonifero das visinhancas
do porto, serra do Bussaco, e moinho d’ordem proximo a aleacer
do sal. 1865.

Greenwood, G. Rain and Rivers, or Hutton and Playfair against
Lyell and all comers. 2nd edition. 1866.

Hauer, F. von. Beitriige zur Paleontologie von Oesterreich.
Parts 1&2. lso8.

Hauer, K. yon, Die ren Kohlen Oesterreich’s. 2nd edition.
1865.

Heer, O. .Die Pflanzen der Pfahthanten. 1865.
Herschel, J. F. W. Physical Geography... 2nd edition. 1862, —

Huxley, T. H., and B. W. Hawkins. An elementary atlas‘of Com-
parative Osteology. 1864.

Kaufmann, F. J. Untersuchungen tiber die mittel- und ostschwei-
zerische subalpine Molasse. 1860.

Keller, F. Pfahlbauten. 6th Bericht. 1866.

DONATIONS. 339
Kobell, F. von. Geschichte der Mineralogie, von 1650-1860. 1864.

Koch, C. Paliozoische Schichten und Griinsteine in den herzoglich
Nassauischen Aemtern Dillenburg und Herborn unter Beriicksich-
tigung allgemeiner Lagerungsyerhiltnisse in angrenzenden Lan-
dertheilen. 1858.

Loriol, P. de. Description des animaux invertébrés fossiles contenus
dans V’étage Néocomien moyen du Mont Saléve. Livr. 1 & 2.
1861-63.

Maack, G. A. Palzontologische Untersuchungen tber noch unbe-
kannte Lophiodonfossilien von Heidenheim am Hahnenkamme in
Mittelfranken, nebst emer kritischen Betrachtung siimmtlicher bis.
jetzt bekannten Species des Genus Lophiodon. 1865.

Martin, J. Paléontologie Stratigraphique de l’Infra-lias du départe-
- ment de la Cote dOr. 1860.

Massalongo, A. B. Saggio Fotografico di alcuni animali e piante
fossili. 1859. °

Ooster, W. A. Catalogue des Céphalopodes fossiles des Alpes Suisses,
ayec la description et les figures des espéces remarquables. 1863.

—_—. Synopsis des Echinodermes fossiles des Alpes Suisses. 1865.
Oppel, A. Der Mittlere Lias Schwabens. 1853. _

——. Palxontologische Mittheilungen aus dem Museum des kénigl.
Bayer. Staates. Part IV. 1865.

Owen, R. On the Anatomy of the Vertebrates. 2 vols. 1866.

Paléontologie I'rancaise ou description des animaux invertébrés
fossiles\\de, la France. Terrain Crétacé. Livraisons 18-21.
Tome vii. Hehinides. 1865-66.

. Terrain Jurassique. Livraisons 6-9. Tome iii. Gastéropodes.
Par M. Piette. 1865-66.

Passy, A. Description Géologique du département de la Seine Infé-
rieure. 2 vols. (Text and Atlas), 1832.

Percy, J. Metallurgy: the art of extracting metals from their ores
and adapting them to various purposes of manufacture. Vol. i.
Tron and Steel. 1864.

Pictet, F. J. Meélanges Paléontologiques. 1863.

Schenk, A. Die fossile Flora der Grenzschichten des Keupers und
lias Frankens. Lief. 1. 1865.

Schoenlein, J. L. Abbildungen von fossilen Pflanzen aus dem
Keuper Frankens; mit erliuterndem Texte nach dessen Tode
herausgegeben, von A, Schenk. 1865.

390 DONATIONS.

Seebach, K. von. Der Hannovyersche Jura. 1864.

Senft, F. Die Humus-, Marsch-, Torf- und Timonithtia als
erzeugungsmittel neuer Erdrindelagen. 1862.

Stabile, J. Fossiles du Lac de Lugano. 1861.

Stenzel, K.G. Zwei ‘Beitrage zur Kenntniss der fossilen Palmen.
1850.

Stoppani, A. Paléontologie Lombarde, ou Description des fossiles
de Lombardie. 1858-62.

Terquem, O. | Paléontologie du systéme du lias inférieur du grand-
duché de Luxembourg et de Hettange, du département de la
Moselle. 1855.

Thurmann, J., et A. Etallon. Lethea Bruntrutana, ou Etudes
paléontologiques et stratigraphiques sur le Jura Bernois, et en
particulier les environs de Porrentruy. 1861.

Visiani, R. de. Palme pinnatee Tertiariz agri Veneti. 1864.

Watelet, A. Description des Plantes Fossiles du bassin de Paris.
Livr. 1-5. 1865.

Zincken, C. F. Die Braunkohle und ihre verwendung. Hefte 1-3.
1865.

Zirkel, F. Lehrbuch der Petrographie. Vol.i. 1866.

[Quarr. Journ. Gzou. Soc. vol. xxi. to face p. xl.

ADDENDUM TO THE ANNIVERSARY ADDRESS OF THE PRESIDENT.

Dr. Grorez ForcHHAMMER was born at Husum on the 26th July,
1794. After his preliminary studies in Latin and chemistry, he
entered the University of Kiel, where he became an assistant in
Pfaff’s laboratory. In 1818 he went to Copenhagen, where he soon
became Oersted’s assistant. In 1820 he took his doctor’s degree, on
which occasion he wrote a treatise ‘De Mangano.’ After travelling
for two years in England, Scotland, the Hebrides, and the Faroe
Islands, he was appointed teacher of Mineralogy and Chemistry at
the University of Copenhagen. In 1825 he became a Member of
the Academy of Sciences there; in 1829 he was named Professor of
Chemistry and Mineralogy at the Polytechnical Institute; and in
1831 Professor of Mineralogy at the University. Since 1851 he was
Director of the Polytechnical Institute, and Secretary of the Aca-
demy of Sciences.

His literary productions were partly chemico-mineralogical, and
partly geognostical, chiefly with reference to the Danish Kingdom
and the Duchies. An important portion of his investigations refers
to the water of the sea and that of springs, wells, streams, and fresh-
water lakes. Many of his works refer generally to natural history,
while others contain views and representations of objects of natural
history.

Dr. Forchhammer was blessed with an unusual capacity for
work, which, together with his rich stores of knowledge, enabled
him to meet the numerous calls upon his time and labour. The Pro-
fessorship at the University, the care of the Mineralogical Museum,
the Directorship of the Polytechnical Institute, the Secretaryship of
the Academy of Sciences, required extraordinary powers from one
man. Moreover, as Rector of the University, he had to superintend
new buildings of great extent, and to make full reports on many
questions referred to him by the Government. He was consulted
scientifically, not only for public, but for many private undertakings,
where his knowledge, his practical talent, and his extreme good-
nature were available. The result was that he was loaded with
honours by the Government, and that he enjoyed the friendship and
esteem of all who knew him.

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.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

Marcu 21, 1866.

The following communications were read :—

1. On the Fosstt British Oxen. Part I. Bos Urus, Cesar.
By W. Boyp Dawxrns, M.A., F.G.S.

ConTENTS.
1. Introduction, 4, Measurements.
2. Characters. 5. Range in space and time.
3. Synonyms. | 6. Relation to domestic races.

1. InrrRopuction.

Since the publication of Professor Owen’s great work on the
British Fossil Mammalia in the year 1846, no addition has been
made to our knowledge of the British Fossil Oxen, while on
the continent Professor Nilsson, of Lund, has described with a
master’s hand those of Scandinavia, and Dr. Riitimeyer, of Basle, those
found in the Pile-works of Switzerland. In the meanwhile a large
amount of information with reference to them has been obtained from
the bone-caves and river-deposits of Britain, and from the peat-bogs
and marls below of Britain and Ireland, for the most part unpub-
lished or scattered about in disjointed fragments through the nume-
rous scientific and archeological journals of the day.

The relics of the food of the Roman legions stationed in Britain,
and of the Romano-British, and the contents of their tombs, and
especially many incidental notices of wild oxen in the historians
from the time of Charlemagne down to the end of the 12th century,
afford remarkable evidence as to the date down to which the wild
oxen lived in continental Europe and in Britain. To collect all these
isolated facts together, and to give an outline of the characters of
each species or variety,-and to define their range, so far as may be,

VOL, XXII,—PART I, 25

392 PROCEEDINGS OF THE GEOLOGICAL sociuTy. [ Mar. 21,

in time, is the object of this essay. The three species which come
under our notice are—l. The Great Urus, Bos wrus of Julius Cesar ;
2. The Small Short-horn, Bos longifrons of Professor Owen; 3.
The Bison, Bos bison of Pliny.

The problem as to the origin of our domestic races of cattle is only
to be solved by a careful examination of each of these three European
fossil animals. Of the three, we shall begin with the Bos Urus of
Julius Cesar.

2, CHARACTERS,

The Bos urus, or the Bos primigenius of Bojanus*, is cha-
racterized, according to the latter, by the concavity of the fore-
head, by the prominence of its orbits, which have not such a for-
ward direction as in Bos taurus, and by the large size of the neural
spines of the dorsal vertebrae. The large horns also have a double
curvature, first outwards, and then forwards and upwards. Pro-
fessor Nilsson}, describing the remains of this animal found in Scania,
describes it as characterized by the flatness of forehead, the straight-
ness of “the edge of the neck,” and by the horns being very large
and long, near the roots directed outward and somewhat backward,
in the middle bent forward, and towards the points turned a little
upwards. Baron Cuvier, on the other hand, writes, with reference
to the skulls of this animal that he had examined ¢, “ The general
contour of the frontal bone, its concavity, and the reentering curve
which bounds it above, and which extends as a crest from one horn to
the other, the acute angle that the surface of the frontal makes with
that of the occipital, the circumference of the latter, the temporal ©
fossa, are absolutely the same in these two skulls as in the common
Ox (Bos taurus).” In the horn-core of the Urus he can detect no
differences of specific value as compared with the former animal, in
which almost every variation of curvature is to be found; while at
the same time the fact that the horn-core of the Urus, after bending
outwards, bends back upon itself a little downwards and forwards,
instead of presenting the regular double curvature of that of the
common Ox, outwards and more or less upwards or forwards, is well
worthy of remark. The common Ox, however, presents every varia-
tion in the size of its horns, sometimes being entirely hornless, as
in a Welsh, Scotch, and Islandic breed, at others having them most
enormously developed, as in the Sanga or Galla Ox of Abyssinia, in
which variety, according to Father Lobos (quoted by Zimmerman,
Spec. Zool. Geograph. 4to, 1778, p. 110), the horn is sufficiently
large to contain more than ten quarts. A walk into a cattle market
will convince the most sceptical of observers that the common Ox
presents also almost every variation possible in the shape and the
direction of the horns. In fine, a very careful comparison of the
skulls of Bos wrus in Britain with those of the various varieties
of Bos tawrus or the common Ox, compels me to believe that there

* "Nev. Act.-Acad. Nat. Cur. xiii. 2. p. 424, 1. 24.

+ Anm. & Mag. Nat. Hist. 1849, vol. iv. ser. 2. p. 257-258.
{ Oss. Foss, t. iv. p. 150, 3rd edit. 1826,

\ 1866. ] DAWKINS— FOSSIL BRITISH OXEN. 393

is no difference of specific value between them, those points of
difference noticed by Professors Riitimeyer and Nilsson proving to
be peculiar to the individual and not to the species, and therefore
useless for classificatory purposes. At the same time, its size,
though inferior to that of the Italian or Abyssinian animal, was far
greater than that of any variety of Bos tawrus, which coexisted
with it in the forests of France, Germany, or Britain, and affords a
ready means of identification ; while it is easily differentiated from
the smaller contemporary Bison by the double curvature of the horns,
their backward position close to the occipital crest, the concavity of
the frontal bone, and the acute angle that the occiput makes with the
frontal region. The quadrangular outline of the occipital region

and the larger size of the bones, the anterior dorsal vertebra being
excepted, are also guides by which to recognize it.

3. SYNONYMS.

The synonymy of the Bos urus is in a state of very great con-
fusion, arising from the fact that the two words denoting two
distinct species, the Urox and the Aurochs, are derived from the
same Sanscrit root, wr, aur, or or, that signifies a forest or stony
waste. The root can be traced through many languages, and still
survives in the Greek dpos (a mountain), the Norwegian ore, the
Islandic urd (the stony desert surrounding the base of the mountains),
and is preserved without change in the old German wr (a forest) and
in “ Ur of the Chaldees.” It appears also in the Ural Mountains,
and also in the canton of Uri, the crest of which is anox-head. At
the annual election of magistrates in the latter place, my friend the
historian of ‘ Federal Republics, Mr. E. A. Freeman, tells me that two
gigantic horns with double curvature are borne in solemn procession ~
to this day. These probably are of considerable antiquity, and were
obtained from a gigantic Urus-bull* that fell a victim to the chase,
in which the German youth in Cesar’s time prepared themselves for
the toils of war, obtaining almost as much honour from the possession
of horns of Urus slain by their own hands as from that of trophies won
in battley. The root also occurs in the name applied to the gigantic
ox of the tableland of Central India—the Gaur (Bos gaurus). With
reference to this, Mr. W. A. Chatto observes, “The word Gau or
Ghoo, as it is sometimes spelt by European writers, appears to be
used both as a generic and specific term in Persia and Hindostan ;
and as it has the same meaning as the German word Kuh, and the
English Cow, it is highly probable that its origin is the same. As
the word ur in Hindostan appears to have the meaning of wild or
savage, the name Gaur or Gau-ur literally signifies wild cow t.

* That the Urus’s horns were used in the Bronze age, and possibly before, is
proved. by Professor Nilsson’s discovery of a bronze trumpet made in the shape
of a horn of Urus, dug from a depth of 6-8 feet out of a turf-bog in Southern
Scania. ‘“Itis more than probable that the inhabitants of the south of Sweden
first used the horns of the Urox for their war-horns, and at a later period made
themselves horns of bronze in the same form as the former.” Op. cit. p. 267.

_tT Ces. Bell. Gall.
{ Nat. Hist. of the Ox Tribe. By George Vasey. 8yo. pence ae p. 103.
25

394 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

The German Urox, Aurochs, and the Gaur of Hindoostan are
therefore etymologically one and the same, and mean primarily wild
or forest ov, but are used to denote three distinct species. To pass
over the latter species of Hindostan, with which we have nothing to
do in this place, the term Awrochs has been restricted to the Kuro-
pean Bison by the authority of Buffon, Cuvier, and Professor Owen ;
the term Urox, or Bos urus, to the species under consideration by
Julius Ceesar, Pliny, the chronicler of ‘The Wars of Charlemagne’*,
and other writers of the 6th to the 12th centuries; also by Cuvier,
Nilsson, and our great naturalist Professor Owen. The Polish
“Thur” is simply another form of the root w, and signifies wild ox.

A reference to Dr. Fischer’s great work (Synopsis Mammalium,
Svo, Stutgardtie, 1829, pp. 497-498) will show the confusion that
exists between the Uroaw and Aurochs in the works of the older Kuro-
pean naturalists, and will obviate the necessity of my giving details
in this place.

The large fossil ox of the Pleistocene period, termed Bos prim-
genius by Bojanus and Professor Owen, differs in no respect from
the Bos wrus of the Prehistoric and Historical period.

4, MEASUREMENTS.

The following measurements show that there was a consider-
able difference in size between the individuals of the Bos urus.
They are all reduced to inches and tenths, for the sake of ease of
comparison. The first skull that Cuvier mentions(op. cit. pp. 150-151,
pl. ii. figs. 3-8) presents a

in.
Width! between the tormecores:of 1e6.8/.00s0 he sescoe ce eeerereee 12:8
s GEDIS eee ees edits islet oR etches Seance ee eee 12-9
Circumference Of HORM SCORE siociantaiveimioncnnhe et ieeeineoake eee eee 12:9
Length of horn-cores following curvature..........00.+-sseeese 27°9
Distance between tet tips. . he. sekesacneee on eee sees ne oe 32°5

Cuvier observes of this skull that, according to the proportion of the
Bos taurus, it would belong to an animal 12 feet long and 6°5 feet
high at the withers.

The dimensions of a second and more perfect skull, dug from the
peat-bog of Saint-Vrain in the canton of Arpajon (op. et. pl. xi.
- figs. 1, 2, 3), indicate an animal of considerably smaller size than the
preceding — |

Extreme length from occipital crest to end of premaxillary...... 25°75
Distance benmeon (6) 07) eR ELAR SO NMS A tes on WES;
Horn-core to horn-Core.....52..-h.dcsececsabeeseo-0 SA EEE peer Ps 5 11:0
Diameter, of horn=Core jab. DaSe) pcs .0e)-eawn ew share nonce ees eee Ree 5D
Distance between tips of horn-cores,:........--.ce--------2-+0s-n¥erse 24:8

Height of occipital crest from the bottom of the foramenmagnum 8°8
Maximum width of occipital surface between the two mastoid

OVO CERTIER) oA Nae SANE: SA Sn Seperate Ri wlgcsunivnani enc oaeine ohne 12:0
Antero-posteriorextentiol palates... -aiccse.dscescustereessses0-ume es 12-08
Length of skull from the foramen magnum to anterior edge of

Premaarallaiesieeaepeses cree mcm beseyeseken See ak aca RMGL ace naceteme 22:05

* Monachi Sangallensis Lib. ii. de Rebus Bellicis Caroli Magni, ec. xi.

1866. | DAWKINS— FOSSIL BRITISH OXEN. 395

This skull is 4 inches longer than that of the largest Bos tawrus in
the Jardin des Plantes.

The most perfect remains, however, are those derived cam the
turbaries-of Scania, described by Professor Nilsson, of Lund*. They
afford the following measurements in inches and tenths i

reupital crest to premaxillary.........0....:cc0s--seesssdassennee 28:33
Horn-cores to anterior edge of premaxillary .................. 25°41
Bate) CONE) OL ONIONE (cg Sere cteelcam «.delea dace nidelaicnsl noe nied daieiwe dwar 15°33
BMEMEUI VE GINOLN-COLE ic deteacs (b4s.cdennaaee + ensrecgeametsiog 26:0
Breadth of forehead between base of upper partofhorn-cores 9:08
e lower part of __,, 12-0]
ii 4 * between orbits, upper part ............6- 12:01
ey lower part0.:4.:. 44.3.1 11°33
Distance between tips OU DOE COLES 5 vale eace «crise salen wel dae 28:0
Circumference of base of horn-Ccore..........ceseeeeeeesenseenees 14:33
Distance between auditory foramina .................-ceeeeeees 12:33
First cervical to last dorsal vertebra .........0....cceeeeseeeees 91°33
Cervical vertebrx ............. Ree ir et Puce aot er pr eee Ee 23°33
Megara ot shoulder-blade: veces. cncersva sachs cadesengraesns dagabes 20:0
PercmenEe Oot CIStA ENE svcaden vides sas ade didsns denne sdoasiose ve 12-0
Length of humerus between articulations .............:0...005 14-0
of BT RGRLSR (oh cace cose n tees econ wacrusleas ad gee teieests, bois oe 14:33
is GE UMMA AMG OLECFANODM: -../25s cs secs okt ie asenssais eet onbes 19°5
Ss RRIBIeRRE My ee ee Dee, Sas Lon oe eee ag Ba. Saceaeaa Geko Beonews 19:0
_ BUTS Pes eas Sacra aN caeot. co nates uaaathcaaaseticdslowesiee ies
3 oP TEENS LUTTE he I PR RN ee eee ee 11:0

Professor Nilsson estimates the length of the animal as being from
11-5 to 12 feet, and its height over the withers as about 6 to 6-5—
an estimate that coincides remarkably with that given by Baron
Cuvier from the examination of the head of a French specimen, which
we have already noticed.

To pass, however, to the remains of the Bos wrus found in our own
country, the first and most noteworthy discovery in Britain was that
of the frontal portion and horn-cores in the bed of the river Avon at
Mellisham, near Bath. The span from tip to tip of the unbroken
horn-cores was 39 inches+, their basal circumference 17:5, and
their length, following their curvature, 36:5. This last measurement
is one-fourth greater than that mentioned by Cuvier as indicating
an animal 12 feet long and 6°5 feet high. Mr. Woods also cites an
instance of the occurrence of a head of this species of a size little
inferior to the head of the preceding, under a tumulus near Calne
in Wilts, and associated with remains of the Deer, Boar, and British
pottery ornamented with right lines. The measurement from tip
to tip of horn-core of 33 inches, and their basal circumference of
15:5, prove that at the time the makers of the tumulus lived in Wilt- |
shire a Urox inhabited the same area of larger size than any of
those mentioned by Baron Cuvier in Germany, or by Professor Nils-
son in Scania.

Professor Owen figures, in the ‘ British Fossil Mammals,’ a skull
fromnear Athol, in Perthshire, derived probably from a turbary. It is

* Op. cit. p. 258 et seq.
t Descript. of Fossil Skull of Ox. By Henry Woods, A.L.S. 4to. London,
1839: p. 29.

*

396 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

36 inches long, the span of the horn-cores is 42 inches, and the
breadth: of the forehead between the horn-cores 10:5 inches*. Dr.
Fleming notices the large size of the skulls of oxen from the marl-
pits underlying the peat of Scotland, and speaks of one in his pos-
session as being 27:5 inches long, with a span of 9 inches between
the bases of the horn-cores, and of 11:5 across the orbits. He
considers them to have belonged to a species of Bos tawrus f.

All the cases cited above, with the exception of that found on
the banks of the Avon, near Bath, which may perhaps be of the same
date as elephantine and leonine remains found in the neighbouring
gravels, are of a date posterior to the extinction of the Mammoth,
tichorhine Rhinoceros, Cave-bear, and other animals character-
istic of the Pleistocene period in Central, Western, and Northern
Europe, and are derived from deposits either of peat or of marl
beneath it, or from tumuli. They are therefore of Prehistoric age.
The few remaining measurements that I shall give are those of the
_ skulls and horn-cores of the same species that boast of a vastly
greater antiquity, and which were associated with the remains of
the Pleistocene Mammals, both in the caverns and in river-deposits
of that early period.

Mr. Brown, of Stanway, to whom we are indebted for the discovery
and preservation of the remains of a large number of Pleistocene
mammals, describes a skull of this species, along with the molar of a
Elephas primigenius, in the drift of Clacton in Essext. Hach of its
cores measures 36 inches in length following the outer curvature,
and has a basal diameter of 6 x 5 inches. Professor Owen de-
seribes a second skull, obtained by Mr. J. Wickham Flower, F.G.S.,
from the drift of Herne Bay, as possessed of horn-cores measuring
along the outer curve 39 inches, with a basal circumference of 18-85.
A remarkably fine pair of horn-cores have also been obtained from
the brick-earth at Crayford, in Kent, belonging to the low-level
series of gravels and brick-earths of Mr. Prestwich. Their basal
circumference is 16°6 inches, and their length, following the outer
curvature, 35 inches. They are preserved in the collection of Mr.
Grantham, to whom I am indebted for their examination. A large
number of other cases of the remains of this species having been
found in Britain may be cited, as in the river-deposits near Erith,
Maidstone, Ilford, Wickham, Brentford, Bielbecks in Yorkshire,
and Fisherton in Wilts, and in the caverns of Kent’s Hole, Oreston,
and many others. As sufficient evidence has been given for the
variation in size of the head and of the horn-cores of the species,
_ their measurements would serve no special purpose in this place.
The measurements of the Jong bones and lower jaws will be given in
a tabular form in the essay upon the Aurochs, or Bison priscus of
Professor Owen.

One point is very remarkable with reference to the development
of the horn-cores and the size of the animal—that just as the -

* Op. cit. p. 512.

+ British Animals. 8vo. Lond. & Edin. 1828: p. 24.
t Mag. Nat. Hist. n. s. 1838, p. 163,

1866. | | DAWKINS—FOSSIL BRITISH OXEN. 397

Urus mentioned by Czsar as “ magnitudine paulo infra elephantos,”
and that found in the peat and in the marl beneath in France,
Northern Germany, and Scandinavia, surpassed the average uncas-
trated Bos taurus of Western and Central Europe in size, so were
they exceeded in size by those that inhabited the same area in the
Pleistocene period. The more abundant food afforded by the vast
prairie grounds of the Pleistocene continent would naturally cause
‘the Pleistocene Urus to attain to a higher pitch of development than
the more restricted range and food, after the submergence of the
Pleistocene lowlands, of the species in Prehistoric and in Historic
times, where, moreover, it would have a hard battle to fight for its
very existence with the most formidable of the beasts of prey—with
man. This is the only hypothesis that I can suggest to account
for the larger size of nearly all the Pleistocene Mammalia as com-
pared with those descendants of them now living in the same area.

5. Rance In Space AND TIME.

That the Bos wrus or Bos primigenius was a contemporary of the
Mammoth, leptorhine, megarhine, and tichorhine Rhinoceros is
proved by its occurrence in the brick-fields of Crayford, in Kent,
already mentioned. Besides the above, it was associated with

Felis spelza. Cervus elaphus.
Ursus spelzeus. Elephas antiquus.
Ursus arctos. Equus fossilis.
Bison priscus. | Arvicola amphibia.

Megaceros Hibernicus.

In the brick-earths on the opposite side of the Thames it is
associated with the Hippopotamus major at Grays, in Hssex. The
associated remains, indeed, from many other localities such as that
given above leave no room to doubt that it wandered through the
Pleistocene woodlands in France, Germany, and Britain with
the other mammalia of the period. A table of the distribution of
Pleistocene Mammalia in my possession proves that it was far
less numerous in Britain than its smaller contemporary the Bison,
or Bison priscus of Professor Owen. In Prehistoric times, after the
Elephants and Rhinoceroses of the Pleistocene period had passed
away,and the Cave-hyenas and Cave-lions had retreated from Western
and Central Europe southwards, it still held its ground in France,
Germany, and Scandinavia; and from the instances cited of the
occurrence of its remains, it seems to have become relatively more
numerous than the Bison, which also survived in Europe, but which,
so far as I know, has not yet been detected in any Prehistoric de-
posit in Britain or Ireland. The case of the skull of this species
‘being found under the tumulus at Calne, associated with the remains
of the feasts and the fragments of pottery of some ancient British
tribe, proves that the Urus was hunted in those early days in Wilt-
shire. The date of its extinction in Britain is, to say the least,
a very vexed question. Professor Owen infers, from the condition
of the remains from the Scotch peat-bogs, that it retained its ground
longest in Scotland; Nilsson infers, from Cesar’s silence, that it was

398 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

extinct in his time; but when we take into consideration the small
area that he saw of the country, and its physical condition, covered
with vast forests and pathless morasses, his silence does not seem to
be of any weight either for or against the extinction of the animal
at that time. The absence, however, of its remains from the very
numerous accumulations of bones of Bos longifrons, Red Deer, Wild
Boar, and the like animals, which were the food of the people after
Britain was interpenetrated by Roman influence, makes it highly
probable that it was, to say the least, very scarce. It may perhaps
have still lingered on in the wilder parts of the country. To add
to the perplexity as to the date of its extinction, William Fitz- .
Stephens, in his ‘ Life of Becket,’ incidentally mentions the condition
of the country immediately to the north of London*. After deseri-
bing the pleasant gardens that the citizens had out of town, the pas-
tures and hills, he says, *‘ Close by there extends a great wilderness,
woodland glades, the lurking-places of wild beasts, Red Deer, Fallow
Deer, Wild Boars, and Wild Bulls” (tauri sylvestres). Whether or not
“taurus sylvestris” be synonymous with Bos wrus in this passage
may be disputed, as it may be objected that perhaps it may mean
only the domestic cattle that were sent out into the woods to get
their own living. On the other hand, the fact of their being classed
under the head of fere, along with the Red Deer, Fallow Deer, and
Wild Boar, read by the light of records of the existence of the Urus
on the continent at that time, inclines me to the belief that they
were as undoubtedly wild in Britain in the middle of the 12th cen-
tury as the wild bull hunted by Charlemagne in the forest of Aix-
la-Chapelle, to be mentioned subsequently. That the Bison is not
meant is rendered almost certain by the absence of its remains from
any British formation posterior to the Pleistocene period. The
smaller Bos longifrons may perhaps be the animal meant in this
passage. Probably, however, the Urus lived in Britain to Becket’s
time in a wild state, modified in size according to its food and the
extent of its range, that of the Pleistocene being vastly larger than
that of the Prehistoric times, and the latter than those few survivors
in the struggle for life when the cultivated lands encroached more
and more on their feeding-grounds and the dread of the hunter was
upon them. The half-wild oxen of Chillingham Park in Northum-
berland, and other places in Northern and Central Britain, are pro-
bably the last surviving representatives of the gigantic Urus of the
Pleistocene period, reduced in size and modified in every respect by
their small range and their contact with man.

On the mainland of Europe Bos wrus was very numerous and had
a very extended range, both in Pleistocene and Prehistoric and
Historic times; while in our own country, insulated from the con-

* Undique extra domos suburbanorum horti civium arboribus consiti spatiosi
et speciosi contigui habentur. Item a borea sunt agri pascue, et pratorum
grata planities aquis fluvialibus interfluis; ad quas molinarum versatiles rote
citantur cum murmure jocoso. Proxime patet ingens foresta (not forest, but
uncultivated ground), saltus nemorosi, ferarum latebre, cervorum, damarum,

aprorum, et taurorum sylvestrium. (Vita sancti Thome, auctore Willelmo filio
Stephani, vol. i. p. 178). 8vo. Hdidit E. A. Giles, Oxoniz.

1866. ] DAWKINS—FOSSIL BRITISH OXEN. 399

tinent, at the close of the Pleistocene it was exposed to exterminating
causes that did not obtain in the far larger and wilder area of the
European mainland ; it was rare in the two latter periods, and pro-
bably became extinct as a wild variety several centuries before the
species (or variety) on the continent was driven’ away from the
Hercynian Forest and the banks of the Danube. In Pleistocene times
it wandered in vast herds over Northern, Central, and Western
Europe, and, according to Bojanus, over Southern Russia, and, in
company with the Woolly Rhinoceros (2. tichorinus) and the Mam-
moth, frequently fell a prey to the Cave-hyena and the Cave-lon.
In the Prehistoric deposits of France, Germany, and Scandinavia
its remains are very abundant, and in the latter district prove that
it was far more numerous than the contemporary Bison.

That the animal was hunted at this early date in Scania is proved
by the discovery by Professor Nilsson of a skeleton which had been
pierced with a javelin. It was found at a depth of 10 feet, at the
bottom of a peat-bog, and “lay with its head downwards; and one
of its horns (horn-cores) had penetrated deep into the blue clay
which formed the bottom under the peat”*. The evidence that the
animal fell by the hand of man is indeed perfectly incontrovertible.

The dwellers on the Pile-works of the Swiss lakes have also left
numerous remains of Bos urus among the bones that have been found
surrounding the rotten piles, in association with other varieties of
oxen, for the discussion of which I must refer to the works of Dr.
Riitimeyer, of Basle.

In Historic times the animal has been frequently mentioned, first
by Cesar, as a dweller in the Hercynian Forest along with the Elk and
Bison. Its name occurs also in the writings of Pliny, Martial, and
Seneca, in passages which must be familiar to those who have studied
the works of Professors Nilsson and Owen, and of Mr. Henry Woods,
who hasdescribed so ably the ox-head found at Melksham, near Bath +.
There are, however, other and later notices of the animal scattered
through the records of France and Germany from the 6th to the
12th centuries, that have not as yet attracted the attention they merit
in this country. The chronicler of the life of St. Karilef, the
founder of the Abbey of St. Calais, happens incidentally to mention
an interview that the hermit saint had with Childebert, the son of
Clovist. It came to pass in this way: the king happened to be
out hunting in the Province of Maine about the year a.p. 540, and
having started a fine ox—rare game in that district—he chased it
with his dogs right into the hermit’s cell, where he found it standing
behind his back. This passage proves two things—that the Bu-
balus or Wild Ox occurred sometimes in the Province of Maine, and

*"Op- cit. p. 264. Tt Op. cit.

400 PROCEEDINGS OF THE GEOLOGICAL SUCIETY. [ Mar. 21,

that this one happened to be tamed by the hermit. There may indeed
be a doubt as to whether the Bubalus mentioned here be actually the
Bos urus; but interpreted by the light of what we know in other
districts respecting the hunting of Bos wrus, I think that probably
it was the animal mentioned in this passage: at all events, the
passage is worthy of note.

In the ‘ Wars of Charlemagne,’ written by a monk of St. Gall, a
remarkable anecdote is told of a hunt in the forest near Aix-la-
Chapelle, in which the king was attacked by a Bos wrus, and in
which, for the first time in history, “‘ hose” are mentioned*. “On
the next day Charles, very tired of the quiet and leisure, prepares
to go into the forest to hunt (Bisontium vel Urorum) Bisons or Uri,
and to take the Persian ambassadors along with him, who, when
they saw these gigantic animals, struck with very great terror,
took to their heels; but the hero Charles, unmoved, mounted on a
very swift horse, coming up close, drew his sword and attempted to
cut off the head of one of them. But when he missed his stroke, the
most fierce beast, rending his sandals and gaiters, and grazing his
thigh with just the tip of its horn, made him a little more cautious,
and then, enraged by the slight wound, took refuge in a most safe
retreat, bristling with thickets and stones; and when all his suite,
to curry favour with the king, wished to take off their hose (hossas
suas vellent extrahere), he forbade them, saying, ‘ In this plight I
must go to Hildegarda (one of his wives).’ And Isambardus, the son
of Warinus, the persecutor of your patron Otmarus, having followed
up the beast when he dared not approach nearer, thrust his lance
between its shoulder and throat, pierced its heart, and presented it,
still quivering, to the king. This deed he pretended not to notice;
and leaving the dead animal to his companions, he returned home,
and called the queen (Hildegarda), and showed her his torn hose,
and said to her, ‘ What reward is he worthy of who has delivered
me from an enemy inflicting these things upon me?’ And when she
answered, ‘ Of every good,’ the king told her every particular; and
haying had the vast (immanissimis cornibus) horns brought forward
as a proof that he was telling the truth, moved the queen to tears
and groans and beating of her breasts.” .. .

It is clear, then, that at this time (the beginning of the 9th
century) Bisons and Uri were still to be found in the forests near
Aix-la-Chapelle. The description of the horns proves that the ani-
mal was one of the latter species, as the size of the horns of the
former is not such as to warrant the use of the term “ immanissima.”
In the remarkable collection of MSS. preserved in the Abbey of St.
Gall is one by Ekkehard the younger, who lived from a.p. 980 to 1036,
and composed a set of graces for the use of the monks, in which we
are indebted to the custom of returning thanks after every dish for
the preservation of the names of the animals they atey. Among

* Monachi arcing Lib. ii. de Rebus Bellicis Caroli Magni. Folio. co
Chesne.) Chap. x

if + Beledlanioned ad mensas Ekkehardi Monachi Sangallensis,” Archzol: Journ.
vol. xxi. pp. 117-186. ‘“ Dextra Dei veri comes assit ‘carnibus uri” (p. 125).

1866. ] _ DAWKINS—FOSSIL BRITISH OXEN. 401

the wild animals, the list comprises Bear, Wild Boar, Red Deer, Roe
Deer, Fallow Deer, Chamois, Wild Horse (Equus feralis), the Beaver
(which is termed a fish, and therefore eatable on fast-days), the
Bison, and the Urus. The Bison and the Urus, then, were sufficiently
abundant in the wilds of Southern Germany and Switzerland at the
close of the 10th century to be used as an article of food, and to be
deemed worthy of a special grace by the monks of that day. At the
close of the next century (the eleventh) the Urus is mentioned along
with the Elk as being met with on the route through Germany taken
by the First Crusade, and the large size of their horns is noted*.
Posterior to this, in the 12th century, in the ‘“ Niebelungen-Lied,”
Tregfried is said to have killed one Bison and four Uri in the neigh-
bourhood of Worms (p. 3775-6), For four centuries after this no
mention is made of the animal; and if not extinct in Germany, it
must have become very rare. Gesner, in his ‘ History of Animals,’
published at Frankfort in the year 1622, gives a figure of the Polish
“‘Thur,” which corresponds exactly in the curvature of its horns
with the wild Urus of Germany, though it is very much inferior to
the latter in point of size. The wild Urus, therefore, probably lin-
gered in the wilder parts of continental Europe till at least the 16th
century ; and having first of all sprung into being in Pleistocene
times, survived the larger of its contemporaries, and is indeed
superior in point of bulk to any of the Pleistocene mammalia that
have come down to the times of history. In Pleistocene, as I have
mentioned, it was larger than in Prehistoric times, and in the
latter than when it was last met with in Poland. The diminution
in size is probably to be accounted for by the gradually diminish-
ing area over which itranged. The area in Prehistoric and Historic
days was gradually lessened by the hand of man and the encroach-
ment of cultivation on its old haunts.

6. Retatrion to Domxstic Raczs.

The question that still remains to be discussed is, whether or not
it still lives in any of the domestic races. Professor Nilsson thinks
that the larger cattle of the Netherlands and Holstein have sprung
from this animal. Baron Cuvier and Professor Bell believe that the
Urus was, in part at least, the ancestor of our domestic breeds;
while Professor Owen thinks that the tame ox of Western Europe
was probably derived from the already domesticated cattle of the
Roman colonists. The evidence, on the whole, inclines me to the
belief, as there is no osteological or other difference saving that
of size between the Urus and the domestic race of cattle, (to pass
over the notice already quoted of the tame “bubalus” being
hunted into the hermit’s cell in Maine) that the larger cattle of
Western Europe at least are the descendants of the former animal,
modified in many respects by restricted range, but still more by
the domination of man.

* “Uris cornua sunt immense concavitatis, ex quibus ampla satis et levia pocula
fiunt.” (Hist. Gest. Viz Hierosolymitane a Fulcone quodam, Lib. i. [Du
Chesne, Hist. Franc. |) ; t+ Op. cit. p. 500.

402 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

2. Further Documents relating to the Formation of a New Isuanp in
the neighbourhood of the Kaimunt Istanps. By Commander G.
TRYON.

(Communicated by the Lords Commissioners of the Admiralty.)

[An abstract of this communication was published in Quart. Journ. Geol. Soe.
No. 87, p. 319, by order of the Council.]

3. Note on the Junction of the THaner Sanp and the CHaux, and of
the SanpeateE Bens and Kentish Rac. By THomas M*Kenny
Hueuss, B.A., F.G.S8., of the Geological Survey of Great Britain.

Ar the bottom of the Thanet Sand there is always a bed of green-
coated flints in a green and rust-brown clayey sand*.

The following observations have led me to infer that this bed is
due to the decomposition of the top of the Chalk after the deposition
of the Thanet Sand :—

1. The flints never show any traces of having been rolled or worn
by the action of water, or broken up and weathered by any subaérial
agency, but are, except in colour, exactly similar to those in place in
the Chalk. °

2. No fossils, except chalk fossils preserved in flint, have been
found in it.

3. Where a nearly continuous bed of flints, or a large tabular
mass of flint occurs, the base-bed of the Thanet Sand seems to be
arrested by it in a manner that would suggest rather the chemical
decomposition than the mechanical erosion of the surrounding chalk.

4. Where masses of chalk are imbedded in the base of the Thanet
Sand they appear to be due to local undermining of the main mass
of the rock, and not to be transported fragments rearranged in a
hollow.

Again, to look at the question from another point of view, it is
highly improbable that it could be otherwise. As water charged
with carbonic acid, soaking through the Thanet Sand, reaches the
chalk below, it must decompose the surface to a certain extent; and
if the water can pass freely away so that new supplies, not saturated
with carbonate of lime, are brought to act upon it, that decomposi-
tion must go on ad infinitum.

The only difference, therefore, between this action extending over
the whole surface of the chalk where covered by Tertiary or later
deposits and that which forms pipes is, that in the case of the pipes
the water is collected at or near the surface into small streams ;
whereas in the other case it permeates the whole of the deposit over-
lying the chalk, and acts more equally on its surface.

There are cases where the surface of the chalk does not appear to
have suffered any great amount of decomposition—as, for instance,
north-west of Rainham, in Kent, where there is very little of this

* For further description, see Prestwich, Quart. Journ. Geol. Soc. vol. viii.
p. 243. See also Whitaker, enfrd, p. 405.

1866. |] HUGHES—THANET SAND AND CHALK. 403

green bed with flints at the base of the Thanet Sand. The junction
may be seen in a chalk-pit in the brick-field north of Moor Street.
But there are local circumstances by which this may be explained :—

‘Ist. There is a bed of clay in the Thanet Sand, as may be seen in
the road-cutting leading to the brick-field; and .

2nd. There is other evidence of a line of upheaval running nearly
east and west through this part of the district, which, in conjunction
with the bed of clay above mentioned, would have the effect of
throwing the drainage off to the north and south, and therefore
partly protecting the surface of the chalk here from the action of the
carbonated water.

Similar reasoning may be applied to explain the local phenomena
of the more westerly part of the Tertiary basin—as, for instance, at
Reading and Newbury, where the surface of the chalk is bored by
Lithodomi to a considerable depth. Here the impervious beds of clay
in the overlying Reading series have probably contributed most to-
wards protecting not only the oysters of the lowest part of the Ter-
tiary beds, but also the surface of the chalk from the action of the
carbonated water. It is known that the clays of the Woolwich and
Reading series allow very little water to pass through them*.

An examination of the junction of the Sandgate Beds and the
Kentish Rag leads to a similar conclusion. In the large quarries on
the north-west of Maidstone, at the base of the Sandgate Beds, there
is a greensand, generally on rubbly Kentish Rag. The thickness of
these intermediate beds varies. It is greater in hollows and depres-
sions, where, we have reason to believe, a larger amount of the Rag
has been removed.

In the brick-fields close to the town of Maidstone the brick-earth
occurs in long furrows of the nature of pipes, in the Kentish Rag.
The whole of these furrows are lined with greensand and rubbly lime-
stone, similar to that found at the base of the Sandgate Bedst+.

Now, unless we allow that the greensand has been derived from
the decomposition of the Rag after the deposition of the brick-earth,
and that the rubbly limestone below it is the same in process of de-
composition, we have only the improbable alternative left that the
irregular denudation which removed the Sandgate Beds previously to
the deposition of the brick-earth left the same thin bed at the surface
over this large area.

There are several interesting questions raised by this view of the
origin of such beds. What do they represent? Do they represent
the periods during which the surface of the limestone has been above
the sea-level? for, except in some peculiar cases, if it were under
the sea, and the water on its surface were at rest, 7. ¢. not constantly
renewed by fresh infiltration, it would soon become saturated with
carbonate of lime, and could remove no more.

_ How much limestone has been removed since the deposition of the
overlying beds? ‘The thickness of the beds formed of its insoluble
remainder is not a fair criterion; for, in the case of the chalk, for

* * See Prestwich, Quart. Journ. Geol. Soe. vol. x. p. 82, footnote.
T See Messrs. Foster and Topley, Quart. Journ. Geol. Soc. vol. xxi. p. 448.

| 404 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

instance, where a large quantity is washed and run in troughs, as is
frequently necessary in the cement-works and brick-fields of North
Kent, it is found that the amount of sand left varies considerably in
different localities. Atthe cement-works about one mile anda half
south-west of Rochester it is very large; near Sittingbourne, on the
other hand, it is comparatively small. (The former is near the junc-
tion of the Upper and Lower Chalk, the latter near the top of the
highest chalk of that part of the country.)

Mr. Prestwich* has speculated on the origin of the green colour.
I would add one note. It seems to occur where carbonate of lime
has been dissolved. We find it, as noticed above, on the decomposed
surface of limestones ; and where lines of greensand or sandy clay
occur in the Lower Tertiaries, there we most often find casts of shells7.

The chief deduction from these observations is, however, general—
viz., that we cannot safely draw any conclusion as to the conformability
or unconformability of a porous formation upon a limestone from an
examination of the line of junction only, since that may be: very
much modified after the deposition of the newer formation.

The unconformity may be inferred from other evidence, as, for
instance, in the case of the Thanet Sand, which, it is well known, is
not the direct successor of the highest Cretaceous strata found in
England.

4. On the “Lowrr Lonpon Trrttartes” of Kent. By Wi1iam
Wuitaxer, Hsq., B.A. (Lond.), F.G.S., of the Geological Survey
of Great Britain.

[Prats XXIT.]
ConTENTS.
1. Introduction. 6. Fossils.
2. Thanet Beds. 7. On the Outliers of Sand on the
3. Woolwich and Reading Beds. North Downs, which have
4. Oldhaven Beds. been classed with the Crag.
5. General relations of the Divisions 8. Conclusion.
of the “ Lower London Ter- 9. Description of Plate XXII.

tiaries”’ to one another.

§ 1. Iyrropvcrion.

Txe following paper is meant to give some of the results of the
Geological Survey work in the Tertiary District of Kent, and to lay
before the Society the conclusions to which that work has led me, in
order that they may receive that criticism which is so valuable to
every observer.

I give results only, so as not to burden the Society with a deserip-
tion of sections, which would be out of place here for two reasons :
—first, because Mr. Prestwich has already described the chief sec-_
tions of the district, and I can therefore refer to his well-known

* Quart. Journ. Geol. Soe. vol. x. p. 244.
+ Perhaps the carbonate of lime neutralizes the effect of the acidulated water,
and prevents its acting on the silicate of iron.

~ 1866.) WHITAKER—LOWER LONDON TERTIARIES, 4095

papers*; and secondly, because a detailed account of all of them
will appear in future Geological Survey Memoirs.

It is also needless to notice earlier authors, as Mr. Prestwich has
given a full list of them.

_ Although the Geological Survey of the district in question is not
yet finished, still so little is left undone that there can be no doubt
as to the general correctness of the observations on which this paper
is founded.

It should be stated that, although the whole of the district is
known to me, I have not myself surveyed all of it, Mr. Hughes being
answerable for the mapping of the country between Rochester and
Faversham, and Mr. Dawkins for some part of the neighbourhood of
Faversham. All the rest is my own work, the unfinished parts
being on the east of Eltham, in the neighbourhood of Erith, and
around Cliffe and Halstow, between the Thames and the Medway.

The more I have learnt of the Tertiary beds, the more have I seen
reason to agree with Mr. Prestwich’s views; and, indeed, all he has

left to do is the filling-in of his outlines, the addition of a few de-
tails which seem to have escaped his notice, and a. change in nomen-
clature in a matter that he looked on as doubtful; in fact I only
differ from Mr. Prestwich in questions on which he has spoken
with doubt. q

The beds between the London Clay and the Chalk, of which this
paper treats, are of far greater interest in Kent than elsewhere, and
for these reasons :—1, that they are there most fully developed; 2,
that their structure is there more complex and shows more change
than anywhere else; 3, that there are many fine sections; and, 4,
that they are almost without fossils in all other districts. These
beds might indeed be well called “ the Kentish Tertiaries.”’

§ 2. Toaner Bens.

_ The indefinite word “ Beds” seems to me better than the more
definite “‘ Sands” or “Clays,” as it is somewhat uncommon for a
formation to have everywhere the same lithological composition ;
and I have therefore used the above name rather than that of
«Thanet Sands.”

(a)7 At the base of this set of beds, and resting at once on the
Chalk, there is always a clayey greensand, with unworn green-coated
flints at the bottom ; to this the name of the “ Base-bed”’ may be
given. Mr. Prestwich has called the like part of the London Clay
the “ basement-bed”+; and I have named that of the Woolwich
and Reading Series the “bottom-bed”§. By using a different
name for each of these marked layers, one is saved the repetition of
the names of the formations to which they belong.

This is the only part of the series which is constantly present,

* Quart. Journ. Geol. Soc. vol. vi. p. 252; vol. viii. p. 235; and vol. x. p. 75.

T The letters a, b, a, B, &c.,and the numerals 1, 2, &c., refer to those by which
the several beds are distinguished in the sections in Pl. XXII.

$ Quart. Journ. Geol. Soe. vol. vi. p. 255 (1850).

§ Geol. Survey Mem. on Sheet 13, p. 23 (1861).

406 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

although it is the thinnest, being often but two or three feet
thick, and seldom more than five. For this reason, and from
the fact that the green-coated flints are unworn, the question
has occurred whether it may not have been formed, In some
measure, after the deposition of the beds above, by the slow ac-
tion of water flowing through the overlying sand, &c., to the Chalk,
dissolving away the latter and depositing clayey matter, salts of
iron (the green colouring-matter), and sometimes allophane. The
occurrence of the last mineral at the junction of the Thanet Beds
and the Chalk has been recorded by Prof. Morris*, who says that
‘it must have been deposited from a fluid or viscid state, not only
after the denudation of the Chalk and the deposit of the partially
abraded (?) flints, which are coated with it, and after the accumula-
tion of the Thanet Sand, but subsequently to the disturbance of the
whole series, whereby the fissures in the Chalk were formed, and in
which the allophane is now found.” I have since found it at the
same junction at Chiselhurst and Faversham ; and I believe that it
occurs at the bottom of the Reading Beds at Northaw, where they
rest on the Chalky.

Mr. Prestwich has noted “ the constant occurrence” of the green-
coated flints at the bottom of the Thanet Beds, “just as they occur
in the underlying Chalk, from which in fact they appear to have
(been) removed comparatively without wear or fracture,” but has
inferred that a ‘‘ powerful but transient action”? must have. been
needed “to uproot these flints from the Chalk ”.

It is remarkable that, whatever rests on the Chalk, there should
nearly always be unworn flints at the junction: thus in the western
part of the London Basin there are flints at the bottom of the Read-
ing Beds ; andin the many places where the Chalk is hidden by the
irregular deposit of brick-earth so common in Wiltshire, Berkshire,
Oxfordshire, &c., the two are separated by the peculiar “ clay with
flints,” as I have called it§, the origin of which my friend Mr.
Codrington, F.G.S., and myself have, independently, referred to the
slow dissolving away of the Chalk by water||. I think it not un-
likely that the “argile a silex”@] of the French geologists (or some
part of it) is the same as our clay-with-flints, in which case, strange
to say, the same name will have been given to the deposit in two
countries and languages. Prof. Hébert’s description of the former
in France** would in great part serve equally well for the latter in
England.

I have before noticed the remarkable conformity between the
Ae
ey Ye:

* Quart. Journ. Geol. Soc. ¥,. xiii. p. 13 (1857).

+ Geol. Survey Mem. on Sheet 7, p. 30 (1864). It was noticed before by Mr.
Prestwich as ‘“‘ hydrate of alumina:” Quart. Journ. Geol. Soc. vol. x. p. 123 (1854).

+ Quart. Journ. Geol. Soe. vol. viii. pp. 243, 253.

§ Geol. Survey Mem. on Sheet 18, p. 54.

|| Magazine otf the Wilts. Archwol. and Nat. Hist. Soc. vol. ix. p. 167 (1865),
and Geol. Survey Mem. on Sheet 7, p. 64 (1864).

€ T have lately (July) seen some of the “argile a silex” on the coast of
Normandy, where it is exactly like the clay so common on our own Chalk.

** Bull. Soc. Géol. France, 2¢ série, t. xix. p. 445 (1862), and t. xxi. p. 58 (1864).

1866. | WHITAKER—LOWER LONDON TERTIARIES. 407

Thanet Beds and the Chalk in East Kent*. Is it not possible that
this also may be owing, to some extent, to the infiltration of waver
along the line of junction, and that the dissolving away of the chalk
by the water may have been stopped, or regulated, by the continuous
bed of flint which there occurs directly below the base-bed? I do
not mean to say that this can have taken place since the elevation
of the country to its present position, but would suggest that such
_ an action would not be impossible when the beds in question were
many hundreds of feet lower, and therefore saturated with water
throughout, and subjected to great pressure from overlying materials.
Should this be true, it will be a case of the same action causing
exactly opposite results under different conditions; the infiltration
of water through the Tertiary beds to the Chalk now (when com-
paratively small) causes unevenness (pipes) at the junction, at least
where that junction is near the surface, whilst it may have caused
evenness when of far greater extent and when the junction was at
a great depth.

Since the above was written, I have found that my colleague Mr.
Hughes has come to a more decided opinion as to the formation of
the bed of green-coated flints after the deposition of the Thanet Beds,
and that he has gone into the question in greater detail than I have,
as may be seen from his paper (p. 402).

Mr. Codrington, in the essay before noticed, has come to the con-
clusion “that the origin of the clay-with-flints is to be ascribed to
the gradual dissolving away of the chalk-with-flints wnder a capping
of drift brick-earth.” .

Just after this paper was read, Mr. Dowker published a note on
the junction of the Thanet Beds and the Chalk, in which he sug-
gests that the bed of green-coated flints may be the result of the
subaérial dissolution of the Chalk before the deposition of the Thanet
Beds. I can hardly agree with this view, but look with more
favour on my friend’s idea, that the tabular layer of flint at the top
of the Chalk may have been formed after*the deposition of the over-
lying beds, and the more so as he has in his collection a specimen of
a green-coated flint partly enveloped in a piece of the whitey-brown
tabular bed. The same idea occurred also to Mr. J. Evans, F.R.S.,
who spoke to me (before the publication of Mr. Dowker’s note) of
the possibility of the layer in question having been thus formed.
This flint-layer occurs further west than is stated in my former
paper, and may be seen at Grays and Purfleet.

Mr. Prestwich has inferred that the layer of unworn green-coated
flints, which nearly everywhere rests on t e top of the Chalk where
it is.covered by Tertiary formations, is ey.vywhere of the same aget.
This may be the case; but it is remarkable that where the Thanet
Beds are present, the Chalk never (as far as I know) shows those
holes of boring mollusks so common where the Reading Beds lie
directly on it, and the occurrence of which at Kembridge, Newbury,

* Quart. Journ. Geol. Soc. vol. xxi. p. 397.

t Geol. Mag. for May 1866, vol. iii. pp. 210, 239.

¢ Quart. Journ. Geol. Soc. yol. viii. pp. 241, 252, 253.
VOL. XXII.—PART I, 2F

408 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

and Reading has been described by Mr. Prestwich*, near Pinner
by my colleague the late Mr. Trench, and near Reading, Amersham,
Chesham, and Maidenhead by myself +.

(6) This bed, which consists of alternations of brown clay and
loam, is local, occurring only, I believe, east of Faversham. It may
be seen at Pegwell Bay, where it is separated from the Chalk by
little more than a foot of the base-bed. No fossils have been found
in it.

This is mostly overlain by, and passes up into, the sandy marl (d),
although another bed sometimes occurs between.

(c) In the railway-cutting close to Bekesbourne Station, east of
Canterbury, there is a little sand below the sandy marl (d), in which
the greater part of the cutting is made; and this I take to be the
same as the Thanet Sand of London and the western part of Kent.
The only other place in that neighbourhood where I saw anything
of it was at Selling.

This fine light-buff.sand thickens westward, and near Sitting-
bourne forms a considerable part of the Thanet Beds. Further west
it gets still thicker, at the expense of the beds above, until, on the
other side of the Medway, it replaces them altogether, and takes up
the whole of the space between the Woolwich Beds and the base-bed,
some 60 or 70 feet. It thins slightly to the neighbourhood of
Woolwich, and then rather more raplily until it dies out west of
London.

No fossils, excepting some casts of eee at Erith (recorded by
Mr. Prestwich), have been found in this bed, which is fairly uniform
throughout its range. At Charlton and elsewhere its lower part is
more clayey, and it passes down into the base-bed.

(ad) Near and east of. Canterbury a grey sandy marl is the most
marked member of the Thanet Beds. It is often rather hard, con-
tains green grains, and is of a slate-grey colour, which weathers to
a sort of brownish-yellow by exposure, the division between the
two colours being sometimes sharp enough to mislead one into
thinking that there are vwo distinct beds.

It often abounds in fossils; and from it have come most of the
rarer specimens in the collections of my East Kent friends, such as
the parts of Crustacea, a few Echinoids, the Turritella, a Solarium,
ard other small univalves, besides many remarkable distorted speci-
mens of Cyprina Morrisiz and Pholadomya cuneata. In the dis-
coloured exposed parts the fossils are nearly all casts, the shell
having been dissolved away; whilst in the less exposed part the
shells remain, but are very fragile. .

This division may be much thicker in some places than is shown
in the section (Plate XXII.) ; for Mr. Dowker found 93 feet of “ blue

* Quart. Journ. Geol. Soe. vol. x. pp. 82, 87, 88, 116.
aera Survey Mem, on Sheet 7, pp. 29,37, 39, 44; and on Sheet 13, pp. 29,

‘

1866. | ' WHITAKER—LOWER LONDON TERTIARIES. 409

clay” above the base-bed in sinking a well at Stourmouth, nearly
the whole of which must beiong to d*.

This marl is more sandy towards the top, and passes up into
the next division.

(e) The uppermost part of the Thanet Beds consists of a fine sharp
light-grey sand, of a slightly greenish tinge, often ironshot, and here
and there with layers of calcareous sandstone, as at the Reculvers:
and Pegwell Bay.

It contains fossils, which near Faversham are sometimes silicified,
as Mr. Prestwich has observed, though with some doubt whether
the bed which contained them belonged to this or to the overlying
seriesf. Mr. Dowker has a large and well-preserved silicified core
from a pit in this sand at Canterbury; it is like that figured by
Lindley and Hutton+, which must have come from this formation
or from the Woolwich Beds, though described (by some mistake) as
from “green sand” near Deal. Mr. John Goodchild, of Sitting-
bourne, has lately found some Crustacean remains and distorted
Cyprine and Pholadomye in the brickyards close to that town;
these, however, must have come, I think, from low down in the
sand, where it passes into the marl below.

From a thickness of 30 or 40 feet near Canterbury, this decreases
westward and thins out before we reach Rochester.

§ 3. Wobdiwice anp Reapine Bens.

(1) The “ bottom bed” does not occur in the most eastern part
of the Kentish Tertiary district; and consequently it is there very
difficult to divide the sands of this series from those of the under-
lying Thanet Beds. ;

At the mouth of the tunnel on the Whitstable Railway at Can-
terbury, the lowermost part of the Woolwich sand is rather clayey
and green, contains a few pebbles, and is more regularly bedded
than the higher parts; and this is all that I have seen to represent
the bottom bed in the neighbourhood. At Sittingbourne, however, -
there is a foot or more of pebbly green sand, and at Upnor rather less
of the same. Westward this thickens, and from Erith to London
the bed consists of from 3 or 4 to 15 or more feet of a rather bvight-
green sand, with flint-pebbles, both in layers and scattered.

West of London, where the Reading Beds rest on the Chalk, the
structure changes, ard insteed of the pebbly light-green sand, with
no fossils but the teeth of Zamne and sometimes an Ostrex, there
are grey laminated clays, with green grains and here ard there
casts of shells§, and dark clayey greensand, with unworn green-
coated flints.

(2) Near Canterbury the Woolwich Beds consist almost wholly

_* The Geologist, vol. iv. p. 213 (1861).
Tt Quart. Journ. Geol. Soc. vol. viii. p. 246, and vol. x. p. 109.
_ £ The Fossil Flora of Great Britain, vol. ii pl. 125.
§ Geol. Survey Mem. on Sheet 18, p. 24. Se
at

410 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

of a pale-grey sand, often of a yellowish or greenish tint, much
false-bedded and rather coarse, whilst the underlying sand of the
Thanet Beds is fine and not false-bedded. Eastwards, however,
the sand of the former gets fine and loses its false-bedding, for
which reasons, and from the absence of the pebbly bottom bed, it is
almost impossible to divide the two; indeed no one would think of
doing so from an examination of that district alone; it is only be-
cause they are sharply separated on the west that one is forced to
try to divide them in the far east.

The “ Corbula-bed” of the coast west of the Reculvers and of
the Richborough section is near the bottom of this division. It is
this Corbula-bed which has yielded the fossils (except some teeth of
Lamne) that have been found in the Woolwich Beds in the eastern
part of Kent, and nearly all of which are silicified. They are
marine, except a specimen of Cyrena cunerformis, which Mr. Dowker
found at Woodnesborough, near Sandwich.

2ais a bed of flint-pebbles in greenish loam, which overlies the
bettom-bed just west of St. Mary’s Cray and at Loam Pit Hill,
Lewisham.

26 is a mottled clay (green, red, &c.), sometimes like the plastic
clays of the west, as in the railway -cutting at Eltham, and some-
times sandy, as on the hills near Cobham. Tn the latter district I
a seen beneath it (in a lane-section) a light-green sand (Section

8, Pl. XXIT.), which may belong to 2, but, on the other hand, may
be the bottom-bed.

It will be seen that 2, 2a, and 26 all occur in the same position ;
that is to say, they each fill up the space between the bottom-bed (1)
and the estuarine shell-beds (4) [not taking into account the thin
bed (3)]|; and as we cannot be sure that we ever see any two of
them together, it is therefore not unlikely that they simply replace
one another; but as I cannot be sure of it, I have thought it better
to give each a separate index-mark.

26 thickens under London into the mass of mottled plastic clays
and sands which have been found beneath the shell-beds in many
wells* (Section 4, Pl. XXIT.), and further west joins the other like
mass which comes on above the shell-beds. .

(3) This bed, though very thin, often indeed no more than three
inches thick, is of some importance theoretically, as from its con-
stancy it shows the amount of denudation which the Woolwich Beds
of East Kent had suffered before the deposition of the Oldhayen
Beds. In that part of the county it is a pale purple-grey sand,
often hardened into small lumps of sandstone, which, as Mr. Prest-
wich has noticed, sometimes show traces of the holes of boring
molluskst. In the neighbourhood of Canterbury the Oldhaven
Series comes on at once above this bed; and therefore either none of
the higher parts of the Woolwich Series ever existed here, or they
have been worn away before the deposition of the Oldhaven Beds ;

* See Prestwich in Quart. Journ. Geol. Soc. vol. x. pp. 142, 143, 148-150.
t Quart. Journ. Geol. Soc. vol. x. p, 110.

1866. ] WHITAKER—-LOWER LONDON TERTIARIES. 411

and it is remarkable that this denudation is quite even, the thin bed
of purple sand or sandstone nearly always occurring at the junction.
In West Kent, on the other hand, tiie denudation has been uneven,
and the Oldhaven Beds rest on various parts of the underlying
series.

I have not seen this bed for some way westward from Shottenden
and Boughton-under-Blean, and near Sittingbourne the junction of
the Oldhaven and the Woolwich Beds is more irregular. At Upnor,
however, there is some sand, whitish at top and purplish below,
dividing the shell-beds (4) from the sands (2); and this, I have no
doubt, is the same as the like bed at the top of 2, near Canterbury.
It occurs also near Cobham (Section 8, Pl. XXIT.), and is very likely
represented near Woolwich by the “layer of hard concretionary
limestone’’ which sometimes underlies the shell-bed*, and by the
clay with calcareous concretions in the same position at Loam Pit
Hill, Lewisham.

(4) The most easterly place at which the well-known Woolwich
clay with Cyrene, Melanie, and other estuarine shells has been seen
is Sittingbourne, where, however, there is no clear section of it.
These clays, which are of a dark colour, laminated, with the shells
in the lines of bedding, mostly stiff, but sometimes sandy, thicken
westward and are well shown at the great Upnor section, where
they are about 6 feet thick, and partly without shells. Hence to
London they are generally rather thicker, but near Abbey Wood are
sometimes cut off altogether by the Oldhaven beds (see section 7,
Pl. XXII.) They reach their greatest thickness just south of Chisel-
hurst, where more than 20 feet of them was shown in the cutting
on the London, Chatham, and Dover Railway. West of London this
bed soon thins out again. In the neighbourhood of Woolwich the
sand below sometimes contains like shells, and may be a distinct bed,
coming in between those numbered 2 and the clay shell-bed ;
though, on the other hand, it may be simply 2 in another condi-
tion. Perhaps, too, there is sometimes another and higher set of clay
shell-beds, divided -from 4 by sand or clay +; but this is a matter
of detail, here of no importance, and in the list of fossils any upper
set of shell-beds is included under No. 4.

(5) At Sittingbourne there is, next below the Oldhaven Beds, a
light-coloured sand with Cyrene, Melame, Ostree, &c., which must
thin out eastward, as it occurs nowhere in the Canterbury district ;
whilst westward it is thicker, as may be seen at Upnor. Further
west, however, it has suffered more from denudation, and is some-
times quite cut off by the pebble-beds of the Oldhaven Series.

In the neighbourhood of Lewisham the top part of the Woolwich
Beds consists of mary feet: of alternations of sand and clay, the

* Prestwich, Quart. Journ. Geol. Soc. vol. x. p. 103.

t At the cliff-section on the French coast westward of Dieppe there are two
masses of the clay shell-beds, separated by clay; and the cliff at Newhaven, in
Sussex, shows a great thickness of the same divided into two by unfossiliferous
sand and clay.

412 PROCEEDINGS OF THE GEOLOGICAL society. [{ Mar. 21
’

_ lower part of which is generally the more clayey ; this bed has been
well named “ striped sand and loam” by the Rev. H. M. De la Con-
damine*. As it is in the same position as bed 5 further east, I
have classed them together, though possibly they may not be the
same.

Under London this part of the Woolwich Beds seems to be often
absent. (See Section 4, Pl. XXIT.)

(56) Many of the London wellst have shown that a mass of mot-
tled plastic clays and sand, of the same nature as bed 2 6, comes on
above the clay,shell-beds. This, therefore, may represent 5; al-
though, on the other hand, it may be a separate bed, and I have
therefore given it a separate index-mark.

West of London 26 and 56 come together, the beds between hay-
ing thinned out, and form the well-known plastic clays and sands of
Reading, &c., where there is nothing but these and the thin bottom~
bed between the London Clay and the Chalk.

§ 4. Orpraven Bros.

Up to this point my nomenclature has followed that of Mr. Prest-
wich ; but with regard to the sands and pebble-beds next below the
London Clay in a great part of Kent, I am obliged to differ from
him—the difference, however, being not as to the position of the
beds, but only as to their relation to those above and below and as
to what they should be called.

Mr. Prestwich has, though with some doubt, classed the greater
part of the pebble-beds of Blackheath, &c., and the uppermost sands
of Upnor and the Reculvers with his “ basement-bed of the London
Clay,’”’ taking them to represent the pebbly loam which occurs at the
bottom of that formation on the westt. To this I objected in a
paper read before this Society about four years ago§, as the layer of
pebbles in clay which on the souch-east of London occurs at the bot-
tom of the London Clay, and is thevefore its basement-bed, overlies
the thicker sandy pebble-beds. Moreover in some places the two are
separated by a layer of sand. ip

I thought therefore that the sandy pebble-beds should be classed
rather with the Woolwich Series, and inferred that the highest sands
of Upnor, &c., would follow the same classification. Since then,
however, I have had the means of learning much more of the “‘ Lower
Lordon Tertiaries,” and am bound to say that the knowledge thus
gained has led me to a greater agreement with the views of Mr.
Prestwich, as I took the first chance of stating||, and to acknow-
ledge that the classing of these sands and pebble-beds with the

* Quart. Journ. Geol. Soc. vol. vi. p. 441.

t Prestwich, Quart. Journ. Geol. Soe. vol. x. pp. 76, 142-144, 148-151.

+ Quart. Journ. Geol. Soc. vol. vi. pp. 254, 255, 261-265, and vol. x. pp. 105-
107, 110, 111, 130 (note),

§ Ibid. vol. xviil. pp. 267-268. The section at Bickley was reopened after
my paper was published, in order to get ballast for the railway.

|| Geol. Survey Mem. on sheet 7, p.24. See also a short account of the Ter-
tiary Beds of Kent in the Geologist, vol. vil. p. 57 (1863).

1866. | WHITAKER—LOWER LONDON TERTIARIES. 413

Woolwich Series in that paper was in some measure a step back-
wards. This was owing to my want of the detailed knowledge of
the subject which I have since been enabled to get, and partly to a
misunderstanding of Mr. Prestwich’s writings, caused by the sense
in which he has used the term “‘basement-bed.” This is the right
place to correct my statement that in the railway-cutting north of
Sittingbourne there was “ nothing like the usual basement-bed to be
seen.” I first saw that section during a sharp frost and after snow,
when, of course, it was neither easy nor pleasant to make a very care-
ful examination, but have since been there under more favourable
circumstances, in the company of my colleague Mr. Hughes, who
mapped that neighbourhood ; and we then found that the lowermost
foot or so of the London Clay was often rather sandy, and contained
a few pebbles, some teeth of Zamna, and alittle clayey greensand—
that is to say, that it had the characters of the basement-bed in
Berkshire, &c. The like thing occurs at the cliff-section west of the
Reculvers, and at some other places, as Mr. Prestwich has noticed.

In the neighbourhood of Woolwich, Mr. Prestwich has classed
part of the pebble-beds with the Woolwich Series, and part with his
basement-bed; but such a division seems to me rather arbitrary,
and it would be impossible to map it. I have been led rather to
look on the whole as one thing, and to separate the pebble-beds from
the Woolwich Series, on which they so often rest unconformably.

It will be seen therefore that, whilst holding to my opinion that
the pebble-beds and the uppermost sands do not belong to the base-
ment-bed, I now think (with Mr. Prestwich in great measure) that
they do not belong to the Woolwich Series—or, in other words, that
they are a separate series, to which, of course, some name must be
given. That of “ Oldhaven Beds” is a good one, and for two rea-
sons,—first because they are well shown at “ Oldhaven Gap” onthe ~
coast west of the Reculvers, and secondly because it is not an ugly
neme—a thing that might perhaps be thought more of in geological
nomenclature with some advantage.

In thus separating these beds from those above and below, I do
not really differ so much from Mr. Prestwich as seems to be the case
at first sight ; for he classes his “ basement-bed”’ not with the Lon-
don Clay” or Upper London Tertiaries,” but with the underlying
series, to form the “ Lower London Tertiaries.” Now the term
oe basement- bed”’ of a formation means simply a peculiar bed at the
bottom of and belonging to that formation; and, on the other hand,
it cannot rightly be used for the bed neat below, in which latter
sense this author seems sometimes to use it. The “ basement-bed
of the London Clay ”’ therefore is the characteristic bed at the bottom
of that formation and forming a part of it.

The difference between my classification and that of Mr. Prest-
wich will perhaps be best understood by tabulating the two side by
side, as below :-—

414 PROCEEDINGS OF THE GEOLOGICAL socreTy. _[ Mar. 21,

Prestwicn, 1850-54. - Proposed CLASSIFICATION.
London Clay. Clay.
( _ ( Thin pebbly loam &c. of the \
western part of the London | B a | London
Tertiary District. Mea . f Clay.
Basement- Thin clayey pebble-bed of | :
bed Lewisham, &c. i )
y of the 4 _ Highest sands of Upnor, the \ _ \
London Reculvers, &c., with pebbles at
a Clay. the bottom. 4 | S
| Part of the sandy ebble-be a
3 of Kent (Blnciiea: Abbey ee a
S | Wood, Shottenden Hill, &c.). iis s
a (Part of the sandy pebble-bed 5,
ao of West Kent (Sunderidge near g
= Bromley, &c.) >
3 Sands, shell-beds, mottled \ NS eas
% Woolwich | clays, lower pebble-beds (un- r A
Ey and 4 fossiliferous and local), and Woolen =a
S | Reading } pebbly greensands of West ae 2
Series. Kent and of part of Hast Kent.- p ogin —
| Mottled plastic clays, sands, | Bede 8 =
&c. of the western part of the : | at
London Tertiary District and | =
\ sands of Hast Kent. y 2
Thanet. © } 9 d eoes Thanet | F
( Seats f Sands, sandy marls, &c. { Bede )

Having, I trust, clearly stated what is here meant by “ Oldhaven
Beds”? a short account of the different members of that series will
now be given.

(a) At the bottom of this series at Upnor there is a thin irregular
layer of pale greenish-yellow sand, crowded with shells (Cyrena,
Ostrea, Cerithium, Melania) and filling small hollows in the underly-
ing sand of the Woolwich Beds. This is not constant, being cut off in
many places by the pebble-bed above, the lower parts of the hollows,
however, being often left as separate patches. This bed is very
local; indeed I do not remember having seen it anywhere else,
though it may occur in places at the great Reculvers section. Pos-
sibly, too, the thin bed of sand with shells which next underlies the
London Clay at the Brockwell Hall Brickyard, Dulwich *, indie be
the same as the above, which it is not unlike.

(3) The characteristic sandy pebble-bed which nearly ene.
occurs at the bottom of this series, varies in thickness from a few
inches to rather more than two feet in the Canterbury and Reculvers
district. At the former place, and for a few miles to the west, it
often undergoes a great change in structure, the pebbles being re-
placed by a mass of sandy brown iron-ore, sometimes 5 feet thick.
Here and there a few pebbles occur below, and scattered through,
the stone, which in some places contains many casts of shells. At
one pit near Boughton-under-Blean all the fossils are of estuarine

* See Geol. Survey Mem. on Sheet 7, pp. 28, 24. '

1866. | WHITAKER—-LOWER LONDON TERTIARIES. 415

Woolwich species (Cyrena cuneiformis, C. cordata, Melania in-
quinata, and Cerithvuwm) ; whilst in another, less than a mile off,
they are for the most part marine (Cardiwm, Pectunculus, Apor-
rhais, Calyptrea, Fusus), but with a mixture of the freshwater
shells.

But a little southwards from these pits another change takes
place, there being nothing but some 30 feet of pebble-beds over the
Woolwich sand at the outlier of Shottenden Hill, the only place in
East Kent where this part of the series thickens in the same way as
at Blackheath, Bromley, &c.

Westwards the pebble-bed is thin, and sometimes there are merely
a few pebbles in the bottom part of the Oldhaven sand; but on the
Cobham hills it swells out again, and from Erith by Plumstead Com-
mon to Blackheath is very thick, as also on the south at Bromley and
Chiselhurst, the name of which last place, indeed, is derived from
the Saxon “ Chesil,’ a pebble.

From Blackheath to Lewisham, a distance of about a mile, the
pebble-beds thin away quickly ; and in the cutting on the Lewisham
and Tunbridge Railway there was to be seen (in 1864) a layer (no
more than from a few inches to a foot thick) of pebbles in sand
capped by another (of the same thickness) of pebbles in clay, the
latter being the true basement-bed of the London Clay.

Although this division of the Oldhaven Series has been here treated
as one bed, yet one cannot be sure that the whole of the thick mass
of pebbles of West Kent represents, or is the same as, the thin layer
of the eastern division of the county; for it is possible that other
beds may come on above, and that the sand of Kast Kent may be
replaced westward by pebbles; but I think that it is the safe and
right thing to treat of it so until the contrary view can be proved,
and the more so as here and there a layer of sand occurs above the
pebbles in the neighbourhood of London.

Most observers must be struck with the very great extent to
which these pebbles have been worn. ‘The flint-shingle of our coasts
nearly always contains flints in many states of wear, from the rough
piece that has not long fallen from the chalk-cliffs to the rounded peb-
ble ; but here all are finished ; at least it is very rarely indeed that even
anything like a subangular flint is to be seen. It would seem there-
fore that these old pebble-beds could hardly have been a shingle-
beach along a chalk shore, for in that case they ought to contain
many flints but partly worn. They must, however, have been de-
rived from the Chalk; and one is led to infer therefore that they
must have been deposited as a shingle-bank some way off shore,
to which no flints could get until they had been so long exposed to
the wearing action of the sea as to be well rounded.

(y) In East Kent a fine light-buff sand forms nearly the whole
of the Oldhaven Beds, excepting at Shottenden Hill, where it is not
shown. Near Canterbury and the Reculvers, this is from 15 to 20
feet thick, for the most part finely false-bedded, sometimes with
layers of clay or of sandstone, and sometimes with fossils.

416 PROCEEDINGS OF THE GEOLOGICAL society. Mar. 21,

Westward, at Sittingbourne and Upnor, it is thinner, and beyond
the latter place is not seen, unless it is represented by the sand
which, as aforesaid, sometimes occurs above the pebble-beds in West
Kent.

A strange form of selenite seems to be characteristic of the Old-
haven sand both at Upnor and the Reculvers ; it consists of crystals
with grains of sand caught up between the thin plates, which gene-
rally cause a peculiar satin-like lustre, but sometimes are in such
plenty as to make the mineral look like concretionary sandstone.
These crystals are of various sizes; they often lie with their longer
axis vertical or oblique to the bedding, most likely from having been
formed in cracks; and now and then casts of shells are made up of
them.

Note on the Fossils from the Oldhaven Beds at Grove Ferry.

I think it right to correct a mistake, of some importance, that has
been made with regard to a section in the Oldhaven Beds, and the
more so as it is printed in the Society’s Journal.

In 1859 a short paper, “ On Some Tertiary Fossils found at Grove
Ferry ” *, was published by the late Mr. J. Brown, F.G.S., who stated
therein that “the beds forming the central portion of this hill above
Grove Ferry would appear, according to Mr. Prestwich’s sections
acura Ne to belong to the ‘ Basement-bed of the London Clay’ (Old-
hayenobeds 2 cu... but many of the fossils which I collected here
PR a appear to have an Upper Tertiary character; indeed some
cannot be distinguished from Crag species.”

Now there can be no doubt whatever as to the age of the sand
in question. It belongs, as Mr. Prestwich has always held, to the
series called “ Oldhaven Beds” in this paper. Its lithological cha-
racter is quite enough to settle the matter: no field-geologist who
had worked at the many sections in the neighbourhood could doubt
for a moment which of the Tertiary sands the pit is in, much less
could one who had mapped the district and traced the continuous
outcrop of each.

As for the fossils, I could never find any but the common shells,
&e., of the Oldhaven Beds; nor could Mr. Dowker, who has been
there often. The section, however, is small, and parts once open
may now be hidden.

Mr. Prestwich having told me that he thought Mr. Brown had by
mistake mixed up some Crag fossils with those from Grove Ferry,
and that the reported occurrence of Crag species at that place was
therefore open to great doubt, I carefully looked through the collec- |
tion, now in the British Museum. The result of this examination
was to convince me that most of the fossils were really from the
Oldhaven sand, and that therefore any mistake in the list must have
been chiefly owing to the wrong determination of the species. The
following remarks show the main points wherein I differ from
Mr. Sowerby’s identifications.

* Quart. Journ. Geol. Soc. vol. xv. p. 135.

1866. | WHITAKER—-LOWER LONDON TERTIARIES. 417

Remarks on Mr, G. B. Sowerby’s List of the Fossils.

The names are in the order of the original list.

. Oorbula Regulbiensis, Mor, From Oldhaven sand.

OOP wD

. Pyrgoma Anglica, Sow. I cannot say what this came from.
. Balanus Chisletianus (new sp.). I did not see this.

Mactra, “a fragment.” I did not see this.

?

Hencklinsiana, Nyst. From Oldhaven sand.

. Nucula tenuis, Mont. From Oldhaven sand.

nucleus, Linn. From Oldhaven sand.
Nos. 6 and 7 may be the same; they are much like the com-
-mon WV. labellata of the Lower Eocene.

8. Pectunculus Plumsteadianus, Sow. From Oldhaven sand. Should

be P. Plumsteadiensis.

. [imopsis aurita, Wood. From Oldhaven sand. Mr. 8. V.

Wood has written to me to the effect that, judging from the
figure in Mr. Sowerby’s plate, this is not the Z. aurita of the
Crag. It looks to me like a small oblique Pectunculus.

. Lucina? “fragmentary.”? From Oldhaven sand. A mere rolled

fragment of a bivalve shell, but, I think, not a Lucina.

. Cyprina Morris, Sow. From Oldhaven sand.
. Astarte elevata (new sp.). From Oldhayen sand.

gracilis, Goldf., var, multilineata, Wood. I cannot say
what this came from.

Burtinvi, Lajonk. This seems to have come from Old-
haven sand, and to be much the same as the foregoing.

. Cyrena consobrina, Caill. -A bad specimen of a small bivalve,

most likely an Astarte, from Oldhaven sand.

. Cardium Layton, Mor. From Oldhaven sand.

. Rostellarva Sowerbyi, Mant. From Oldhaven sand (Aporrhais).
. Trophon subnodosum, Mor. From Oldhaven sand.

. Pleurotoma, “imperfect.” From Oldhaven sand.

. Pyrula nodulifera (new sp.). Idid not see this from Grove

Ferry; but there are some good specimens from the Oldhaven
sand of the cliffs west of the Reculvers in another draw of
Mr. Brown’s collection.

'

. Purpura tetragona, Sow. Not from Oldhaven sand; but must

have got into the collection by mischance.

. Clavatula brachyostoma, Wood? From Oldhaven sand (in a

piece of Cyprina).

. Buccinum concennum (new sp.). From Oldhaven sand. Looks

much like a London Clay Fusus (unnamed ?).

. Chemnitzia elegantissima, Mont. There is in the collection a

shell labelled Chemmitzia which may have come from Oldhaven
sand; but being small and without matrix, it is hard to say.
The same remark applies to No. 25.

. Odostomia, “like O. plicata, Mont.”
. Wassa reticosa, Sow., var. costata, Wood. Not from Oldhaven

sand. Marked as Buccinwm costatum in the collection, into
which it must have got by mischance.

418 PROCEEDINGS OF THE GEOLOGICAL society. [ Mar. 21,

27. Natica Hantoniensis, Sow.? From Oldhaven sand.

28. cantenoides, Wood?=WN. glaucinoides, Sow. From Old-
haven sand. This seems to be the common Eocene J. la-
bellata, Lam., which also=JV. glaucinoides, Sow., this last
name seeming to have been given both to a Crag and to an
Kocene species.

29. Bulla concinna, Wood. I did not see this.

30. utricula, Nyst. From Oldhaven sand.

31. Dentalium, new sp.? Perhaps from Oldhaven sand.

32. Helix, ‘‘adhering to a broken Fusus.” The latter is from the
Oldhaven sand; but the former is a recent species, and
clearly came from a modern freshwater deposit, like that of
Copford (Essex), or from a valley-drift, like that of Chislet,
close to Grove Ferry (see Prestwich in Quart. Journ. Geol.
Soe. vol. x1. p. 110), and has stuck on to the Eocene shell
by chance.

33. Ringicula. I did not see this.

34. Valvata piscinalis, Miller, “in sand within a Cardiwm Lay-
ton.” This seems to be nothing but the broken top of a
Natca from the Oldhaven sand.

30. Liamax. Source uncertain.

I cannot help doubting others of the determinations in the above
list, besides those to which I have therein taken objection. A few
of the fossils, however, were new to me.

There are some small otolithes in the collection, which seem to
have been left out of the list by mistake. I have also got parts of
the scutes of a Turtle and the teeth of Zamna in the same pit.

§ 5. GeneraAL ReEations oF THE Divisions or THE “ LowEr Lonpon
TERTIARIES”’ TO ONE ANOTHER.

1. The Thanet Beds are the most regular of the three series. They
steadily thin away westwards; whilst eastwards from their central
district, near Rochester, fresh beds come on above, and partly perhaps
replace the sand (c), giving the whole a more clayey character.

Wherever a good section of the junction with the Chalk is to be
seen, that junction is even ard does not show unconformity. There
is indeed no str atigraphical proof of unconformity between the
Thanet Beds and the Chalk.

IT must quote some remarks of Mr. Prestwich, which aie seem
to differ from the above. ‘“ Extensive and deep wear of the Chalk
evidently took place before the commencement of the lowest Eocene
deposits. In the neighbourhood of ......... Pegwell Bay, Upnor,
Woolwich, . >... . Reading, Newbury,,....... «.. , and Alum Bay, the
Chalk invariably presents a worn though not very irregular surface,
and is strewed over..... with those peculiar green-coated flints.
This mass of flints, although generally not above 1 or 2 feet thick,
in itself indicates a wide destruction of the Chalk”*. I think that
Mr. Prestwich will now allow that any irregularity that occurs at

* Quart. Journ. Geol. Soc. vol. viii. p. 256 (1852).

1866. | WHITAKER—LOWER LONDON TERTIARIES. 419

the junction, is owing to the formation of pipes after, and not to
the wearing away of the Chalk before, the deposition of the beds.
Moreover, if Mr. Hughes be right in accounting for the formation of
the bed of green-coated flints*, it follows that the destruction of Chalk
needful for its production also took place after the deposition of the
Thanet Beds. Of course the process which would effect this result |
would alike efface the signs of conformity ; and therefore the evenness
of junction may be owing to this, and not to conformable deposition,
as said before (pp. 406, 407).

2. The Woolwich and Reading Beds, though far more constant in
their presence, are less so in their structure. In the far east they
pass into the sands below, whilst on the west the two are sharply
divided, and the pebbly greensand of the bottom-bed sometimes rests
irregularly on the light-coloured Thanet sandt. West and north of
London the Reading Beds lie immediately on the Chalk, as is also the
casein the Hampshire basin. I think, therefore, that we should be pre-
pared to find this series make a like overlap southwards from the
mass of the Kentish Tertiaries, and should not be surprised if outhers
of it should be found resting on the Chalk of the North Downs.
Now on the hills just north-east of Otford there do occur (besides
the loamy mottled brick-earth) masses of bright-coloured mottled
plastic clay, just like that of Berkshire, &c., associated with the
sands which Mr. Prestwich has classed as Cragt.

3. The Oldhaven Beds are the most local, the most uniform in
structure, and the most irregular in occurrence of the whole. Mr.
Prestwich long since noticed the way in which the pebble-beds
rested on a worn surface of the Woolwich Series§, sometimes indeed
cutting off almost the whole of the latter (see Sections 6, 7, 8,
Pl. XXII.); and near Chiselhurst I have lately seen the former
cutting through the clay with shells (4), the pebble-bed (2 a), and
the bottom-bed (1), until it rested on the Thanet sand (c). If, then,
we ought not to be surprised at the Woolwich Beds overlapping the
underlying series and resting on the Chalk of the North Downs, still
less so should we be at finding the Oldhaven Beds in that position.
Here, again, Mr. Prestwich is before me ; for, from having found some
of the peculiar green-coated flints of the ‘‘base-bed” in the Old-
haven sand near Herne Bay, he infers that ‘it is probable that the
denuding action acted not only on the..... upper part of the un-
derlying (Woolwich) series, but that it in places extended to the challe
qsely’? ||.

There seems to be another reason why the Oldhaven Beds must
have somewhere reached to the Chalk; for else how is one to account
for the great mass of flint-pebbles which they contain ?—a mass too
great to have been derived from any beds between the two, none of
which, indeed, contain anything like that amount of flints.

* See above, p. 402.

+ See Prestwich, Quart. Journ. Geol. Soe. vol. x. p. 101.
t Lbid. vol. xvi. pp. 323-824,

§ Ibid. vol. x. pp. 106-107.

|| Lo¢d, vol. vi. p. 277.

420 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

In_the eastern part of Surrey there are some Tertiary outliers on
or near the crest of the Chalk escarpment*. These consist chiefly of
masses of pebbles, and are not shown on the Geological Survey Map,
as,when working in that district some years ago, I was led to take
them for Drift, not being then prepared for those overlaps in the
Tertiary bed¢, of which longerstudy has shown me the existence ; and
I now think that these sandy pebble-beds belong to the Oldhaven
Series. There are a few small outliers of the same in Kent, and also
Se like that associated with the pebble-beds at Shottenden

A long and close examination of the Tertiary district of Kent has —
led me to think therefore that its structure tends to show that
there may have been a southerly transgression t of the Woolwich Beds
over the underlying Thanet Beds, and still more of the Oldhaven Beds
over both.

The transverse section in Plate XXII. may serve as a diagram of
the geological structure implied by the above theory. It does not
show an unconformity between the Thanet Beds and the Chalk, but
rather one in the midst of the Lower London Tertiaries, by means of
which their highest member overlaps the others and rests on the
Chalk.

For the sake of simplicity no outlier of the Woolw'ch Series has
been shown, but only the greater irregularity caused by the overlap
of the Oldhaven Beds.

§ 6. Fossrzs.

Although this paper is founded wholly on geological evidence, apart
from that of fossils, yet the latter have not been neglected, either in
the field or at home; and the accompanying list covtains, I believe,
the name of every properly recorded fossil from these beds. The
authorities from which it has been compiled are as follows :—

(1). The many lists scatterec through Mr. Prestwich’s papers in
vols. vi., vill., and x. of the Quart. Journ. Geol. Soe.

(2). The lists in the Geol. Survey Memoirs on sheets 7, 12, and
13.

+(3). Prof. Morris’s ‘Catalogue of British Fossils,’ 2nd edit. 1854.

+(4). The Monographs of the Paleonxtographical Society, by Mr.
F. E. Edwards, Mr. 8. V. Wood, &c.

(5). The ‘Catalogue of the Fossils in the Museum of Practical
Geology,’ 1865.

(6). The list given by Mr. G. B. Sowerby in the paper by Mr. J.
Brown, Quart. Journ. Geol. Soc. vol. xv. p. 133 (see pp. 416, 417).

(7). The lists by Prof. Forbes and the Rev. H. M. De la Con-
damine in the paper by the latter in Quart. Journ. Geol. Soc. vol. vi.
p. 440.

* See Prestwich in Quart. Journ. Geol. Soc. vol. viii. p. 257, and in the
‘ Waterbearing Strata around London,’ pp. 135-86 (1851).

+ This word may perhaps be better here than ‘‘ unconformity,” as our notions
of conformity and unconformity are not yet as clear as might be wished.

t The names in the list have been corrected according to these works.

1866. ] WHITAKER—LOWER LONDON TERTIARIES. 421

(8). Mr. C. Evans’s note in the ‘ Geologist,’ vol. vii. p. 84 (1864) ;
and a few other short notices of fossils.

It is not, however, wholly made from the above published works,
but has been largely added to from unpublished lists, in my Note-
books, of the collections of Mr. G. Dowker, F.G.S8., Mr. J. Reid and
the Rey. Dr. Mitchinson (Canterbury), Mr. J. Horsley (given to the
British Museum), Mr. J. G. Goodchild (Sittingbourne), given to the
Geol. Survey, and Mr. J. Marten (Ensinge), also in part given to
the Survey, besides many notices of fossils found whilst working at
the Tertiary beds of Kent. Of course I cannot hold myself responsi-
ble for the right identification of the species in the published lists ;
each observer must answer for his own determinations. Some of
these, no doubt, are wrong; but that is not my fault, and I shall be
glad to have corrections and additions.

Sometimes I have been unable to state in what particular bed a
fossil has been found. This, again, is not my fault, but is owing to
the fact that authors are somewhat careless in giving information as
to the exact position or locality of the fossils they find: thus many
specimens are recorded simply as from ‘* Woolwich Beds,” whilst of
others one can learn no more than that they are ‘‘ Lower Eocene.”
I am sorry to say that the last case often occurs, just where it is
most to be regretted, in the elaborate monographs of the Palonto-
graphical Society “On Eocene Shells,” which, whilst being almost
perfect from a zoological point of view, sometimes are of little use to
the field-geologist.

The classification of the large groups follows that of Prof. Huxley
in the ‘Catalogue of Fossils in the Museum of Practical Geology,’
1865, p. lxxv.

4°

ie

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

List oF Fosstts FRoM THE BEDS BETWEEN THE LonpoN CLAY AND THE CHALK,
WITH THEIR RANGE UPWARDS INTO THE BASEMENT-BED OF THE LoNDON
Cray, Into THE Lonpon C1Ay, AND INTO BEDs ABOVE THE Lonpon Cray.

[Those species marked ¢ are so named in the Monographs of the Paleontographical
Society, and those names marked + occur in Professor Morris’s ‘ Catalogue of British
Fossils,’ 2nd edit. ].

i
| oars = | g Oldhaven | Woolwich and on
3 Beds. Reading Beds. (EastKent).
° $3
| feele fes|a
y ete 2 Abas
Names of Fossils. 4 fo [Se ile. fst] 2S le SS
B >i Ss Cio pi fro | Vc & =
26 |28 22/55 (22 [24/4 [Fa] |e
Be |e] 2° 153 |2s[2e| 6 [ee] < |=
ao] S18 [om |ss]20| 5 |sala | &
= sj 2 < Ls for =| By = =
5 ois 83 |‘o aS 3 | 3 S
J =s i 0) om DRs|m | a oa)
Kingdom ANIMALIA.
Subkingdom VERTEBRATA.
Class Mamata. | |
Coryphodon ...... eed ade Beriee ead de *
tDidelphys (?) Colchesteri, ‘Charles-| | /
WOT GAAS BA Sed re ee © peoeee eee * |
|tHyracotherium cuniculus, Ow. ...|...... ee lee
Lophiodon, or panne s etaes
eee eee oT ae See SB ae Se Br Aes br AS *
Bones .. ene eee eee) Ae ey cae Reverd Pde *
Class AvEs. |
one:(pnalaneewlyes.s. deessnaccncclccocc deste Pewee eeacdan a *
| Class Reprints. |
Chelonia. Bones .......:.0..00+00- Be Peer ee = % |cncsedl -% Apsensehaee
Fragments of carapace ...|.. oe 1 eens x
Crocodilia, remains of (Ow.) ....0-]......|....0. “4
Scutes ......... Beer eo sidoe a eee ees. bce Seen leaene * \
Lacertia, remains of (Ow.)...... a eee Ee aa is
tPalxophis longus FOU. cecesn--scas{uas ee ee ?
Class Pisces.
Edaphodon ......... Re eet ANS ee pe Revie irre’ Prato as § die cee
\tLamna contortidens, 4g... soe le eae “gy Peee * *
ase ae dubia, Aq. 2. ee ee thee eee ee? Cee! oe ? ? 5 *
i elemans Ags? Ye. 0.3L te eee ee *
AV Opi, AG). sisccc a! etimns wane eee te eee ?, 2?) |]
(?sp.) teeth . Bier owen eerie oat Ge ee ee ey fees x | * | x
Lepidosteus (vertebrae), 2 apres Bor be Meee Bees, (cess maar: (- nn
pelts ft ECL. tape eee Be eee eee Pee ?
Repidotaniminar? «..<0.ie--sntae-s y apeleee! RUCPS Dare! me, O:
Myhobatis (frasments): Jc. 2s---«-|sas.ca|apececf-ane=4Be-==>- oe x
Ofodas: Seber ie een cone seem efi Cele ee a. % val
Fish (broken up). One fairly per-
fect skeleton got by Mr. J. Mar-
ten, at Ensinge, now in the Mus.
of Pract. Geol. . Se EOE BERS fee dees] tse Eel aee Ses Bees Pe Ree
Bones, scales, teeth, or vertebree .. oe Eee x]x | xix | «| «x Px
Otolithes eeeeeeeeeee eeeetese eeertrreae eer sf oe ee eeereer ¥
{

1866. | WHITAKER—LOWER LONDON TERTIARIES.

Names of Fossils.

Subkingdom MOLLUSCA.
Class CEPHALOPODA.

Nautilus (2 specimens, one found
by Mr. J. Evans, F.R.S., near
Reculvers, the other by Mr. J.
Marten at Ensinge; both in

Betta, Pract, Geol.) .....00000+|.seceeloueeeafeeers: Bee laut Bes aatsi

Class GAsSTEROPODA.

(Including classes Pulmogastero-

poda and Branchiogasteropoda
of Huxley.)

(2 iL. | oii ae
tAporrhais Sowerbyi..................
tAuricula pygmexa, Mor.

Buccinum (?) ambiguum, Desh.,

and “new sp., large and glo-
bose” (Prestw., Q. J. G. 8. v1. 297)

— concinnum, G. B. Sby. (Grove

re HERI EE: ) ccnreaderianesesane

{Bulla concinna, Wood? (Grove| |

errygere p. 418.) ...ccc.ceveess.
utricula, Myst (Grove a ea

see p. 418.) Sree A ccnmaaigh eee Kane
tCalyptrza trochiformis, Lam.......
tCancellaria leviuscula, Desh.

2) aa ee
tCassidaria oar Brand .........
f— striata, SOY. ...ceeceereeees

— crenulatum, Desh. Fo Ran Nie Rae ale ea Ree

t—— funatum, Mant. (including
Cryartapile, D2sh.) ........000005-

= i 00 Cn Ree Ree! HB eka
| LC 0 Pe een nee Bae

t{Chemnitzia elegantissima, Mon-
tagu (Grove Ferry, see p. 417.)..

, or Hulima, ‘“‘a very small sp.
From Thanet Beds, (Prestwich,
Q. J. G. 8. viii. 248.

tClavatula brachystoma, Phil.?
(Grove Ferry, see p. 417.) ......

tDentalium nitens, Sdy. ............

”

—— sp. | aaa ERR EE ec ecuack loc sbsleaessaBecss- Stee
——, small sp.(? =D. nitens)......)....0-)...6--feeeee Pees:

tEulima?, or Rissoa?; see also

al SuaVeharhaUhtate Gane Oho is °C Na a Yn Vi Pei an:

Pass up

Clay.

Basement-bed of London
| Sand, &c. (Central

Above
London Clay.
Into
London Clay

eee ersleeeere

epeesesl(ssere

see terleeeeeste esses

Ps Ce rs |

ees ed

ree ee Ce

| Oldhaven
Beds.

& East Kent), y.
Pebble-bed (West

eeeeee

Kent), B.
Shell-beds, chiefly
clay (W. Kent), 4.

|

2K

*K

2K

eee verteee ese
eee eee e sees

Woolwich and
Reading Beds.

| Sand (E. Kent), 2.

Sandy Marl, d.

Bottom-bed
(Berkshire), 1.

Sand, e.

seeeee

Ce ae ee

K
.
*
3K

5

Pe ee ee ee

VOL, XXII,—PART I.

A24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

Oldhaven | Woolwich and

Pass up E Beds. Reading Beds. (E. Kent.)
jo}
= .[£s|2 |e2| 4
Names of Fossils. Z sPISE|Ealse| S| a rs
S| #/20|fgleci ss] g [ed 3
29) .O18 [sel S3s.-| = lek
Salgale [Sel em |2e| & | ae im
<3 Hotes jd Bic {a~| woe o
S) oF Ss ie a = ei 3 om 3
= H YA R Ay NMo| mM |AU mR
tFusus complanatus, Sby.............|...6+- ae ore aa
pradatus; Sby ei. ie. dea ste ad.2 [tees debe ae pieces enone: *
a Tatts, SOY. <1. bs 20 sthacces tense d|Raew cdl Weeeeedbcneas c x%-I x
planicostatus, Wei... .b. c.lhee-s Mts open eee se - *
T subnodosus, Mor. tc, .1.tecccdeaccedtees. Pee esse * ae eee ees
it buberosus; Og: Uicgeet be teens cfea see e 1% PR] 2 Lee
F SDs. swe tiecs Mosse eeaeee thus cou |theesapEee ee % PO% [OR hectic ee
Helix Gt) | PAS SERIE ETa tae ta aa haes wate des ae Moire hes
tHydrobia Pe MGR 6. Sakis SRP ACRE Getescc! hades x | x
t Websters Mor, isckicss. th c<albessesleone Sh oe aes *x | ?
MiaTAT AK 70) aes Bonccatior “en tecees = Beane Ieee A Saat |saseee *
tMelania inquinata, Defr.......... Salas waleaeee Wee x | *
tMelanopsis ancillaroides, Desh.?...|......|.....qheeeefeeeeee * fx
i brevis, ShG2s: oi ce. ych bee aed Soe dee ene ne ie
rf bucemoides; WG cae. seo bteesse eines eee pee ate ntoeene * | x
subcarinata ? "bs. seekers skenkocnecs sane ape ee mee Boe Hanae %
Subfusitoriiis 22a y.seeee can ieeces Meson ements Peoeecl a INE
Metula juncea, Soy. (=Buccinum| ~
JUMCCUTT) 9 be. cata cee ancs mess CN aie ae Pic *
Murex, foliaceus, IVE? 0. 2.cyeces eee dens sie csealews Kay oe
trNatica catenoides, Wood (Grove
Merry, see ol Gy: ence vaca rateace ss eenec ances ff %
i Hantoniensis, Linn.(orPilk.?)| * | x | * | x
t labellatia, Wi@iia is Belk eccnes x {| # > * |] x
iT patula, Lam.? (from the
Thanet Beds).
T subdepressa, Mor. (=Am-
pullaria), sere: ech de ttn se ctenect speeeesslben ea peace % ) oe Vere % >| aoe
——— (small) sp.). .doeccd.tucsescscwes Po Re eee ear fad veel.s ssafieeecohaneeeeae rea
TNeritina concava, Sby....... 1s teipiais He foveal tees *
if Consobrina |e. 2) l.desscs es vaeadee ees eee eee aap
t—— pglobulus, Defr.........ccceceete fees Ne eee eel esas x | x
pisiformis, Mr. sxts sb eaccs ateee ame ots ae eoaeel oe ee
vicina; DeWeese se a ee ek
AVA OSEONIIA oie bo we AGE aw gk sede eee gs Anke ek LE eReeed COREE x | *
Paludina aspera, Michaud (?=P.
Desnoyert; Desh.) «. .decves.vesees-[ sae eceae ee ecnmeeeee eae eee *
tT lenta, BRANES oe) ee eee *
ae » Btond. var. G,-IMOr. <. ec... aeocss ere nee x | x
MUGORA, DONA. 2), cicccxarnt on duns Bes rcs eee Geta oe soe
Patella, Ws plc seessseanas eeesscbase ee Meee Re nee aso fotos %
Pitharella Rickmanni, Edw. ......|...... Thee Cee Poe * | x
ttPlanorbis hemistoma, Sby. ...... Cae ce eae es x | x
les yaeatias, MDGS. 9. Sesiciss Vocus Ae en ee few ats , A Release *
tPleurotoma acuminata, Sby.
(Grove Ferry, see p. 417) «......J..0s.: ae Vee *
iN COMMA, SO. esos seccbe east x | x fx fx
MRE ree as Gacrty. ole CREE Coens. Peeooe x Lox
tPseudoliva fissurata, Desh. ........Jeccecc|ecceadQeecsstpecceee *
i" semuicostata, Desi. oc. ate-. + dans. ae ay. | PO i:

1866. ] WHITAKER—LOWER LONDON TERTIARIES. 425

Oldhaven | Woolwich and

Pass up Beds. -| Reading Beds.

Names of Fossils.

Clay.
Sand, &c. (Central
Kent), B.
Shell-beds, chiefly

& Hast Kent), y.
clay (W. Kent), 4.

Above

London Clay.
Into

London Clay.
Basement-bed of London
Pebble-bed (West
Sand (H. Kent), 2.
Bottom-bed
(Berkshire), 1.
Sand, e.
Sandy Marl, d.

Pyrula nodulifera (G. B. Sowerdy,
Weer. 8. Zy. 186)).2..2...1..58.. eae Wea Leese
T—— Smithii, Sby. ........ cece fec eee %
i lg MCS Be os acd ica es * | * f
BOPP Cath on scat sive icc qecathiwnnafesas odes roe AAG oat
TRingicula “ turgida, Charlesworth

(and from Thanet Beds, Prestw.

Sea. 8. Vi: 248) .....s....- x | %
PRM eres cE woven tnd hsoa cleans ed|s ove’ ae
EGHEPOR, BP. ...i.0-..0i. cebagtine ss ie sales coment ee |

-~— (see Eulima)
TRostellaria lucida, Sdy. (? Apor-

rhais Sowerbyi, see Prestwich, Q.

Or Gtr Vie BOW ewes kan esssndsesees Tei al
PER e besitos carats seh vere cabenesetls acess i
, or Aporrhais (Pr estwich, Q.
Cre Vill, DAS)... ck cuvcseessvsclewdovades cass oe | Se ee, Meroe eee iar te Oe.
tScalaria Bowerbankii, Mor..........)..0.0-[.0c0e. ee ee ret) (ee er sis sal

SESPIE Us tietes ono Weingut saint Mace ae es ceatinla ses
Seikvioni = nee oY Seer | SOS 0 ARON Pabeaeh ater fe ‘Heep & aheaalexnctalie a84 16852 septa sar ee *
PEEOUINIE acres eisdvact eben ‘5 Cane eee Teese ee A, cSnwcliecies Pieters Neb tok esd toaeatens *
Ocisdi': bo ean BR seme ceny ate cre eehc wane ' |
PPRMEREINE J 22s eacinednss scabs. +eve Se aiai Tire: Sere eee. eee 4
ttVoluta denudata, Say. ....... Pecsaieaschae ©

hath

Class ConcHIFERA.

JL) LEDLIG) SS SERA ee a ea ee Teer: Leas %
Tp Areas Gepressa, SOY. ..i..ccccecesesfreeees ? :
t Dulwichiensis, Hdw. .........]...++- eis: (emery: U aeeea[ees oe %
MI RACCTIIANIA = igi nes Gli orsoadtess ahs saudleveece Gece: Picea *

%
*
x
sl

BD.
Astarte Burtini, Lajonk. (Grove
Ferry, see p. 417 eS eee © Ts caeWviones
——= domacina, SOY. .........-.0ceceee[eoeees ‘ae
elevata (G.B. Sby., seep. df... |e veee- i.
gracilis, Goldf. (var. multili-
neata, Wood). (Grove Ferry,
BREET chee ccsecs.scctess eee (ners, Pee oat.
tenera, Mor....... Bo RS ie | ae eee a ecsedbacteatl cs SaepeweeSalesed ssl oees x x
SEES ME Chachi ves sii sdant¥iasvtciicced{essencls aul
207 UIET SY ae Oe eee | ee fox |
Byssoarea Cailliaudi, Fp oem ee |e Pts Beats slianine te *
re€ardium Daytoni, Mor. ............)s....- baaaeal
rT PUNT, SOY: .s.005 seks vcnes EP) Ges *
t—— Plumsteadiense, Shy. .........)....4. *
t—— semigranulatum, Shy... aeeertes Rnae x |
, 8p. (one, or both the last two sae Bore Seether. By iad Besoee clas Whaat lovee al evanng eerie
tCorbula Arnouldii, Nyst .. Seba eMie is AB ais 5 . ; x
i globosa?, Sdy.......... Pye cates ee ae oe eee

*

426 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 21,

: - Oldhaven | Woolwich and | Thanet
Pass uP : Beds. Reading Beds. BactKent)
em Teele few|

Names of Fossils. Ele ~ e Br eal 2s S| age rs
S Splo pou oA Ss! Gg [ss sl

oS ole Wee) oe|as| 3 1a a

Pealsale 33 ToL os | S | oe =}

sol|solg S| eM Pee| CS Teepe]

4Qvintsio folie [ay| = | Sahota

B) Sia (se\3 [fe € | Sea

4 = ies) io) Ay No) M |QU] wm mM

Corbula Hencklinsiana, Myst.

(Grove Ferry, seep 4072) Vas23. hoc satassdeeee

t Regulbiensis, Mor. ............ Cease! OOO Be Gk Dee ae * | x
Crassatella, sp. (From ‘Thanet
Beds, Prestw.,Q.J.G.S. vill. 248. )
tCucullza decussata, Park. (=TtC.
C¥ASSALIIA, LIOH0-)). 2hdueewa vagtioe cat Waser «eiccasedeaes ac [eee a ane ae Pee errs ia
fCyprina IMOrrisi, S07. Gacccresssiveslenceclecone At A NOR. bane. fecspecl eas eee * | ¥
it plata, S00. nenve+. tess moeaneeslbecees rae Goce Genoa Aannes lea cae ees |
li@yarenta cordata, Mann penne s-cacleondaslenesseireenee po eee
i cuneiformis. Fér. (and in sand
below clay shell-beds, Woolwich,
Preston. @) ids GeiS, LOW) ee. sclheeess
if depercita, SGe. i b8.c. sca scncllavonoalnncercl eee
Dulwachiensis, ech 7001s. sews leecasepe ase ebtentec coats
(6 ne hye] BNW 0125) CAnRpes Aaa ermal nebies caeaerul Lesdee Wisascils ncn
intermedia, Mell.............. Fase Tefe ns eral stiles aoleceteis SN

t obovata, Sby.? (?=C.cordata}| x |......J-.-...

t-——= tellimellla, (HEA. co iiSss sect Sacies adda cleweeac[mawecese Be afonse. NaS selene
, new sp.?, shape of C. cordata,

banded like C. Dulwichiensis. :

Wmdeseribed (1/172) iva tecstcneslea cereal oeaes ieee ia oer
tCytherea convexa, Brong. _(New-

MA VET, BOUSSER) 5,.1-einaic': Newtenic’ ile leaiopesloncel (Beecaeefeceeulnctniae

levigata (var. a?), Lam.
(Prestii GJ \G.S. Vie 201) pool teneeeieeeaes
t Oblique; esi. ccaasascecet ome: x | *
orbicularis, Hdw. (wrongly
taken for C. Bellovacina, Desh.).|......|...... Clee eres Ix | *
—— ovalis (var.?), Shy. (Prestw.
Qed Gi. Sails LO e204) in: anion asta Meee?
Dreissena serrata, Mell. .......... iit eesit ie ease eM Eciacarece Meat nee tee
fGlyemmeris ubuprensis; ors. us ecleserecBh es: $ieides alemenee | eseene ie aad
HISD cocen be doss piesieivaleiseioacllan sila east ftccseat ent, MMEmeese
, or Panopeea.......
eheda substriata, Mor. oie... ec.meneletlae vaca leacnesteesesephe saci atest ofcceyeeleeee a tema *
tLimopsis aurita, Brocchi (Grove
Kerry, see poll.) c.ceccaeesecene He Nat beakbesdns
Tiithodemius,? (bores), ...cccun saee-n-leaces sleeves ges) betbocdl arenes Msecc’
Lucina (and from Thanet Beds, Peg-

well, Prestw. Q. J. G.S. viii. 248)|......).....Peeee es
Mactra (a fragment). (Grove

Ta ae SSG) CELUI (R | ie ae acepimebcrin| | CeMSsllsntindl Katiodn

ttModiola depressa, Sby. ......s00+0-{eeseee *

F CORBA MMOL Tae si obi a sicions ool dase eo goeoae| roses AE owls

ip legen, MSO Brae ceengeenoene’ =a) a (eae Pee eae
ti—— Mitchell or. eee gucie«-|gesuea| sewing) Ho Reece ers

tt simplex, Sby....... Rabie andes

fii subcarinata, LQ, ......se0+s.eeeees %

1866. ] WHITAKER—LOWER LONDON TERTIARIES.

Past ope ne Oldhaven | Woolwich and Hhopet
3 Beds. Reading Beds. (EastKent)
°
| 3.[ss\2 [es| 4
Names of Fossils, eke oles ES\Ealsee| S| - rs
at (oh OMCs a eb oy eee z
S| sla |ot| seles| § | 38 a
oO oP ls So] .2 a Su: Bec =|
Salsa] S [2al\sefoe| Sl ea
29] 8o1s8 of | BN See AB
SSIES [Balis [Sel BBs 5
S| Sl4 [2° )2 [24] 2 |eé| 2 |
SEEMED A 060k ba'e'sipinicclaeeceeee'awivenlicces. (yan en
ttNucula Bowerbankii, Sby..........]...... MEI ey Poesewe ls ta. fevtee [hr onaclpete te *
t cardioides, Hdw.('Thanet Beds,
Pegwell).
REE DES iss ccs eeessuvst actos onele Pre Cone b seven] %H PH feeeeeefeceas. *
t pretence, WO0d. .....3.cc0ses0-leasseelece AY So | gee
margaritacea, Lam. (?=N.
RUMI ISUYS) accu ceccs sees osanesies. 7b be Peewee Fe tec amemen|ics selene s+ *
nucleus, Linn. (Grove Ferry,
G0). Ua 6) % |osceeapeoeees *
t proava, Wood. (Bishopstone
(? what from), Palzeont. Soc.).
{—— sextans, Hdw. (Thanet (?)
Reculvers, Palzont. Soc., ? from
e or 2).
t striatella, Wood ...... Ssaweeninsiuicesuleesss peebaes *
{—— tenuis, Montagu. (Grove
[2S See On YS) ee Pe care. cae %
{—— Thanatiana, Kdw. (Thanet
Beds, Pegwell, Palwont. Soc.,
?from d or é).
Ol, ee aieheuch an Gierit Seitisiva Paiva x | x x | * | %
ttOstrea Bellovacina, Lam. (inclu- .
ene Oe ediilina, S57/.)).....c0000c.le0desslereres x [ x x f *
Z cymbuloides, Wood.
eC, DCS. 6... dane suseaves|eecevaltvadeifeoesasPecesssteeces: _%
‘i elephantopus, Sby. (Mr. S.
V. Wood tells me that he believes
this to be the thickened upper
waive a: ©. gipantea) ............13..... oa | Cee eae aaa *
lateralis (see Prestwich, Q. J.
BR EE) cccicccucehrenstenscesedels Os ceed Eee Seen Bane Cecil ae nen oa ee %
tt flabellula, Lam, .........000+.- di | Oe al Rene! Gee aaa? Fee lenen es *
t pulcherrima, Wood. (Given
simply as from Reading by Mr.
S. V. Wood, Paleeont. Soc.).......)...... ? | *
t{t—— pulchra, Sy. ........c cece eee elec eee (ie | tee GRBs a (a A ee:
tt TEMETE SOY... se deescanesees: (se. Bae eae al tise! (ted lenude %
ee Ene deere ee ee | ae Can |e a Rm hd a * | %
tPanopeza granulata, Mor. Seal mereealeaasadisadensPiodeos lean astbaaee *
Mee MMEHIA, SUY. cb cocsese-cnlevs cos x fx Pox
tPecten contubernalis, Wood (no-
ticed simply as from Herne Bayby
Mr. 8. V. Wood, Paleont. Soc.)
{tt 21) SSE CLOTTEDIY (Cla Res |e eee ee eer ene eee Mee Sos leccooste
ttPectunculus brevirostris, Sby. ...|...... x fx Px | x
Hi GECUASAINIS, SOY. Vee. ove. 0.c 0 (F0ae0- * | x
+t—— Plumsteadiensis, Shy. ......|......|...06 x fx | x
{——-terebratularis, Zam. .........|....../eeeeee Ze) | dace a ata ie oa We ng *
TPholadomya cuneata, Shy. ......... oop cele S864 Coroud | Heke Maser! Aleeee) Resone esecice) - occu | %

—

428 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Names of Fossils.

Pass up

B

&

22

ae

ae

°

P|

tPholadomya Koninckii, Nyst? ...|......
margaritacea, Sby.? .......-|.+.

9 sp. @eeeceseeeeneser eet eseeecrese er eeeeoe

Pholas, iS pacasaisuesaoelgelen ie amectelsepete| deesex

PINNa, /S Pe awn eededeesor ea seeaseegeec st. ues

ftPsammobia Condamini, Mor.......
tSanguinolaria Edwardsii, Mor. ...
Saxicava compressa, Mdw. (MS.)
(From Thanet Beds, Prestw.,

Q. J. G. 8. viii. 248.)
SOLU, (sais <atisenacaocsncestesucceticent
MOMMA Pkiecenshacer<aninc cet
TTeredina personata, Desh, .........
, large and undetermined sp.
(PM sperconatia)) Mscsschs..ssaeate
TTeredo antenaute, Sby. ............

9 VNe eeseece ecPOaeesesess ere Geno lon

sp.
?thracia, oplata S74... accor odds
tUnio Edwardsi, Wood ..........0....

t— Solanderi, Sdy.? .............65 z

{—— subparallela, Hdw. (U. Desha-
yes, Prestw., Q. J. G.S. x. 118)

pS DO- Oe aueelone eevee cubnecenceta.ott:

Venericardia ? ce h OO oc ee beesecercccne| **

Class BRACHIOPODA.
itLingula tenuis, Sby. .........10-0+-

Class Ponyzoa.

'Flustra weresenesteorace Bec oreeeeeeneeeos|s

eoeeeseeeeeioe

senses

eacces

secsee

eacees

eeceee

eeceoe

se ecoe

aecearls

tecece

eee eee

Bees eeleo

¢Lunulites urceolatus, Zam.......... *
Polyzoan, undetermined ........-...|...«»

Subkingdom ANNULOSA..

Class CRUSTACEA.
@aneer, sp......)- Lota nacees eeoeeeas
{tHoploparia Belli, M‘Coy ...... ae

Pa OCORYELES | oivcwcasss sense tne smewes

Order Ostracoda
(or Entomostraca).

{Candona Richardsoni, Jones ......
Cy pitis som Cythere, Se..sp.6 cs. sre. ns
tCythere Kostelensis, Reuss ..... bis
t (Cythereis), “sp. undeter-

mamied. ’? (/OM¢S) a tace-mageccse ska”,
tt—— | (Cytheridea) Muelleri,

MM UNSE ccunap sean Relates ciate <3

eoneee

eles waee

secece

eerteoes

eeeeee

[Mar. 21,

z Be uaren Woolwich and Beds
9 eds. Reading Beds. e
3 a (B. Kent).
A
=| ms i 5 C
« PR Te faet| %
ae aS ov om r~ °
-| 33 as! Es ‘ag 4 ei as)
Piooiesianl oe] © isa ae
mae! 4 Zs ats Sal oo =|
Og $45 Afro.) cs | 2.5
ee. Seen Ae (ea mips =
Bale |28|as]22| & | g3 a
rHra § oO Lo 2 ee) ae) as co]
dia iso3] 2 AO q SO =I
Ot s = o bt 3 oqaa} 3
=e ies) WM Ay kM mM Aw mM
Le Petone alae eentolcecas «Ay we sectioe’sey Gln cee nme *
Se. | Nese (Ae mane |e ee ee
eeoeee *
PO, Rare! De mas % : iad
arate! Remar] boeiieee ey ee *
RAS PEAR BUI See ua elaallogeacie x%
SHARE (ane) eee Pcl 3 eee +
nations *
eeee * ee@eoe * eeoe e@onee *
* e ees * e@eveon *
Sere eoomeae ee e eeseee *
Se ADS ae dereriae ae Ube alee
AGRoON Kanone! DaOmcall sear % lec. cessane Se +
Ge iflagelavavore Bavevone vel ianeoovevers deere HE Hieveretenersie erate *
Ste. eee POA ecco KieceWese
eeoceace te@eeee &R0C eee *
Andon Hoots foeootiaarood | os
poooed booord Godda Dy *
Saeed % Liv seeclsscdecfe ane eels satel eee eee iE
ebe *
eeos eeseeen eeoseeeo * * % eseee *
eeeeoe eeeee eeee ? Y
arelelaisisi sialaie Aon8 Mee BS vo, epoca Reveroteele * * *
GAoecs) Moco! orcs *
* *
Panera aeevoe Haeaee PEs MAMANG ERA eilarerae Koscas Se
acetal! Manes SOG Baricoailoe. cies AGO Aan *
Baton ee AA] GOES nee eee
Sea) Rares] Gannealls seve %
ee » eee @eeeriseeeee *
oSeooG Goose Acotae * * Recs *

I

1866. ] WHITAKER—LOWER LONDON TERTIARIES.

429

Names of Fossils.

Above
London Clay.
Into
London Clay.

+Cythere (Cytheridea) Muelleri,

Miinst., var. torosa, Jones ...... PE eee eee Seo cf
t—— (Cytherideis), STAC 0 CS Ree SAeee oan een a aoe

POPP OC ee eee HORE HEH HE THEH ROH T EET E BOOK pera eels snes rteeeseorbensees

[c. ey Reuss, C. pli-
cata, Miinst., and C. Wetherellii,
_ Jones, have been recorded b
mistake as from the Woolwich
Beds; they are Upper Eocene
species. See Prof. T. R. Jones’s
“Tertiary Entomostraca”’ (Palee-
ontograph. Soc.), p. 26.]

Order Cirripedia.
fBalanus Chisletianus, G. B. Sby.

(tava Merry, see p, 417.) ....0-|..ccccloceeesPeeses:
eM ola esic'c sia heicethwn ciel cece cle cnceefesceesPueoaes

Class ANNELIDA.
tDitrupa plana, Sby sy: Poet ivseasassbe, ccs x

Ms aie cies sa je dos s68Ss20s'e ly ccyoaltassoafrccess es

Class EcHINODERMATA.
MEAT oe snc co eiciaccnnsas+savess

tOphiura Wetherelli, Ford. .........

ee re ere er ard <

Hemiaster Bowerbanki ............|............

Cs coer cry

f Oldhaven }
Beds.

Basement-bed of London
Clay.
Sand, &c. (Central
& Hast Kent), y.
Pebble-bed (West

clay (W. Kent), 4.

| Shell-beds, chiefly |

MME SEOs oie hates sini 2g cde vie'g hoc ad oe eds «: ere poe oe

Spatangus (?Hemiaster Bower-

banki), Prestw....... Boro oral Peet UIE ied:

Oh iC Oe ae AR ole

Subkingdom OCELENTERATA.
Class AcTINOZzOA.
Coral, small ......... li: ea ai
Subkingdom PROTOZOA.
Class SPONGIDA.

Class RHIZzoOPoDA.
Order Foraminifera.
TCristellaria oe Linn., var. pla-}

typleura, Jones .. beammeuceyesedy Whim fe stactd nial taeme 36 “oa sane ae
PAG DISETINA, SPO” ...00csece ved sedsyinns TANNCS Sar Seren SOtene PRryt fx

tNodosarina (Cristellaria) Italica,

Defr. (=C. Wetherelli, Jones) ...|...... *
tNodosarina (Nodosaria) raphani-

strum, Linn. (=N. bacillum,

gS Prerrerce rpc 4: eo ae ee %

Ps Ce a

Woolwich and |
Reading Beds.

Sand (H. Kent), 2.

seers leeeeerseeooe

eleeeseoe

(a) From the ironstone of Boughton-under-Blean.

Bottom-bed
(Berkshire), 1.
Sand, e.

eoeove

sec ee epee tess

Cr ee

Thanet
t Beds
i (H. Kent).

| Sandy Marl, d.

~w

430 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

Oldhaven§ Woolwich and

Pass up 8 Beds. Reading Beds.
Che
i 5. 23 Cae
Names of Fossils. seISS | EdfsS! S] ou ns
S| Bl2olo3/se[e5| Slee |
= Laoeed 1 oO 3s
col ella fee| 2513. | 4) | ane
Sa esig [@s/as[4F| & | get s | o
4a("ele leslie jae 2 |2aeae
fe) Offs 53 o = 3 3 oa 3 8
4 ei fae n Py NS) Q |AvI wm mM
Polymorphina lactea, W. & J. (=P.
ampulla, Jones, and Globulina
OF authors): sche hse see ote Sa ey (eae! Woe Ree ee [soso] , See ?
T Rotalia, Beccarit?. Wii. wea alone eiescs de ede ee ee *
Mextitlantita soa. Meuse: Soeeeaesesees terre? Seana Hesiad Ramer scrcra| ecaane *
Truncatulina lobatula, W. § J.
(=Rosalina Marie, Jones) ...... % |. acne) eee *
LIncerte Sedis.
Nidulites (London Clay and Thanet
Beds).
Kingdom PLANT ZE.
Carpolithes (Rhytidosporum,
Elpoker) ovum Brong... 2oc.30\ a5. selenns elec ee
Zarniostrobus macrocephalus, Lind.
& Hut., a silicified cone (see P+)
AQQ) cca vetiancsios'aes Aaey/nneasisseasecta| is vj.shGete seb arap ef oeee ae eee cl tee eee *
Wome CastiOn io. 5. tose ee aoe eos cl eek Ce HER 4d lndea nC eee Beer *
Leaves, impressions Of ..2..25..4.:1:4|s-0134|seve0s Oe) eore| cba %* | *
ECU =VESSEIS isto icedut i ace me seesen ae. * x | x
WiGO dl. aisle sak op ane n genet eewideedeticae| aa gee Neneae a aeeee an Bese es wate x | *

Besides which, impressions of leaves occur in the “ striped sands ”

(5) at Lewisham, and many plant-remains have been found in the
lower part of the plastic clays, &c., at Reading. (See Prestwich,
Quart. Journ. Geol. Soc. vol. x. p. 88, pl. 4.) These latter have
been more lately named by De la Harpe as follows (in the Geol.
Survey Memoir, on sheet 10, pp. 113, 116), although perhaps it
would be safer, with Dr. Hooker, to leave them without specific
names for the present (note to Mr. Prestwich’s paper, p. 163) :—

Dryandroides Prestwichii, Heer. Grevillea Heeri, De la Harpe.
Ficus Forbesi, De la Harpe (ranges Laurus Hookeri, De la Harpe.
up into the Bagshot Beds). Robinia Readingensis, De la Harpe.

— Prestwichii, De la Harpe.

* The above List does not refer to Kent only, but is a record of all the
fosdls from the basement-bed of the London Clay and the Lower London Ter-
tiaries of all parts of England.

§ 7. On THE OvriieRs or Sanp on THE NortH Downs, WHICH HAVE
BEEN CLASSED WITH THE CRAG.

In 1857 Mr. Prestwich read a paper to this Society “On the Age
of some Sands, &c., on the North Downs,” in which he inferred that
the beds in question are of Lower Crag age *. The following re-
marks on this ae are made with the view, not of giving a

* Quart. Journ, Geol. Soc. vol. xiv. p. 822.

1866. ] WHITAKER—LOWER LONDON TERTIARIES. 431

decided opinion on it, but rather of showing how careful we should
be in doing so.

Mr. Prestwich’s reasons for classing these sands with the Crag
are, that they are different in structure from the neighbouring old
Tertiary beds, and that many of their fossils are like those of the
Crag. Now it has been shown, in the foregoing part of this paper,
that there are irregularities in the Lower London Tertiaries, by means
of which outliers of the upper and middle divisions occur resting at
once on the chalk, without the presence of the lower division, the
Thanet Beds, and also that those divisions often change their struc-
ture. May not, therefore, the peculiar features of these outlying
sands be explained on the supposition that they are transgressive

parts of the Woolwich and Oldhaven Beds ?

I should not venture to make this suggestion were the fossil-
evidence more trustworthy. In Mr. Wood’s list, appended to Mr.
.Prestwich’s paper, the name of every species is followed by a note
of interrogation; and, in the words of that paleontologist, “ the
most that can be said is, that there is a stronger resemblance in
these fossils to the shells of Crag than to those of any other forma-
tion.” Since the publication of the above, fresh fossils have been
found by my colleague Mr. Hughes and myself, but they do not
throw much light on the question. All are in the state of casts or
impressions, and are therefore hard to determine. There are amongst.
them specimens which many paleontologists would at once refer to
Crag species, especially perhaps a large Tellina exactly like 7. Bene-
denuvi (?), and a Panopea like P. Faujasit ; others, however, would
do equally well for Eocene species ; and some can hardly be classed
as of any other age than HKocene—for instance, some specimens of
Phorus quite like P. agglutinans, a Cyrena cuneiformis, and some
examples of a small Nucula (which Mr. J. G. Jeffreys, F.R.S., tells
me is quite unlike any that occurs in the Crag, whilst it seems to
be rather the Eocene WV. minor). When discussing this question, I
haye sometimes been met with the statement that the finding of
the large Zerebratula of the Crag (7. grandis) in the Lenham iron-
stone settles the matter; but against this there is the fact, pointed
out to me by Mr. Charlesworth, that this shell has been recorded as
occurring in Eocene beds in England, under the synonym of 7. bisi-
muata, by no less an authority than Mr. Davidson*. It seems,
therefore, that we cannot get much help from the fossils. I would
add that our knowledge of those from the Kentish Tertiaries is yet
far from perfect ; fresh species (both new and recorded before from
higher beds only) often turn up; so that some of the anomalies of
the Lenham list may perhaps be explained when the fossils of the
older Tertiary beds are better known.

Another element of doubt is, that the fossils occur only in the
ironstone of some pipes at Lenham, none having been found in the
larger masses of these sands at Paddlesworth &c.t—and yet another

-* Monoer. Paleont. Soc.
_+ My colleague, Mr. Topley, has lately found a cast of a bivalve (Cyprina?)
in a field on the hills above Folkestone.

432 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

in the fact that fossils from a bed of sand below the London Clay
have been mistaken for Crag species (see pp. 416-418); for if old
Tertiary shells in fairly good preservation show such a likeness to
those of the Crag as to be mistaken for them, how much more
likely are we to be led astray by mere casts and impressions, such as
those from Lenham ?

Since this paper was read, there have appeared two abstracts of a
note by MM. Cornet and Briart “ On the Discovery in Hainaut, below
the Thanet Sands, of a Limestone with a Tertiary Fauna”*, most of
the species being allied to those of our Barton and Bracklesham Beds ;
in other words, there is a Middle Eocene fauna at the bottom of the
Lower Eocenes. Surely this should lead us tobe careful in deter-
mining the exact position of Tertiary beds by their fossils alone.

_ Those who agree as to the comparatively modern age of the sands
on the North Downs are at issue as to their exact position. Mr,
Prestwich refers them to the Lower or Coralline Crag. Sir C. Lyell ¢
has thrown them down into the Miocene ; and, last of all, a foreign
paleontologist has lifted them up higher than before, as may be
seen from the following translation, for which I have to thank Mr.
Jenkins, the Assistant-Secretary :—‘‘ Moreover the iron-sandstones
of Kent, which Lyell misquotes as Miocene, contain no single typi-
cal Miocene species, but many which are referable to species charac-
teristic of the Upper Crag—a fact of which I have convinced myself
by an inspection of the collections of Mr. Prestwich and of the Geo-
logical Survey ; these beds must therefore be considered Pliocene ¢.

it seems to me that Dr. von Koenen is somewhat rash in saying
that these beds must be considered Pliocene; he has seen the fossils
only, and not the beds they came from ; but he has told me that his
opinion was backed by the late Dr. S. P. Woodward, an authority

second to none in the determination of recent and Pliocene shells.
Mr. 8. VY. Wood and Mr. Charlesworth, however, say that the fossils
cannot be determined with accuracy, as they are only casts.

With regard to the placing of these sands in the Miocene System
by Sir C. Lyell, I cannot help remarking how that age seems to be
used in England as a sort of harbour of refuge for Tertiary rocks,
Wherever there are Tertiary beds of which the age is doubtful (that
is to say, which are not capped by any other deposits, or are capped.
by drift only), those beds have been, at one time or other, called
Miocene—for instance, the Bovey Beds of Devonshire, the Hempstead.
Beds of the Isle of Wight, and the Leaf-beds of Mull. Moreover,
when Tertiary formations are classified by their contained plant-
remains, the worst of all fossils for such a purpose, the odds are
greatly in favour of their being called Miocene. Bovey, Hempstead,

* Geol. Mag. vol. iii. p. 174, and Quart. Journ. Geol. Soc. vol. xxii. part 2.’

a
“+ Elements of Geology, 6th edit., pp. 233, 868 (1865). T believe that Sir
Charles Lyell has since given up this opinion, and now looks on these sands as
Crag.
t “Die Fauna der unter-oligocinen Tertiarschichten yon Helmstadt bei
Braunschweig,” by Dr. A. von Koenen, Zeitschr. der deutsch. ae Gesellschaft.
vol. xvii. p. 461 (1865).

1866,] WHITAKER—LOWER LONDON TERTIARIES. 433

and Mull are also in this list, together with beds in other parts of
the world.

It should be understood that I do not venture to assert that the
‘iron-sands of Paddlesworth &c. are Eocene, but only suggest that,
in the absence of good paleontological evidence, one might look on
them as of that age. The great difficulty in the way of classing
them with any of the old Tertiary beds of the neighbourhood seems
to be, that their fossils as a group are not like those of the latter,
but (as far as the Hocene species are concerned) seem rather to be
more allied to those of our Bracklesham beds, or perhaps of some of
the Tertiaries of the Continent. I can see no difference in the con-
dition of the fossils which would warrant the inference that some
have been derived from older beds: those that have been referred to
Crag species are in just the same state as the Eocene forms.

For the present, therefore, it would perhaps be well not to com-
mit ourselves to any theory; but should clearer evidence of the Crag
age of the fossils be given, either by the finding of better specimens
or by the further examination of those already found, I shall be
glad to take Mr. Prestwich’s view; and if this note on the subject
should be the means of bringing forward such evidence, by drawing
further attention to the question, its author will be as well pleased
as if he could himself make out the age of the doubtful beds.

I take this chance of putting right a mistake made in a former
paper * (where, by the way, I adopted the Crag theory) in saying
that Mr. Godwin-Austen classed some outliers of sand on the Chalk-
hills of Surrey as Lower Bagshot. He has always looked on them,
and on the Kentish outliers too, as Lower Hocene, as also has my
colleague Mr. Bristowy.

§ 8. Concruston.

From what has been said above, and from a study of the sec-
tions in Plate XXII., we may gather the following facts amongst
others :—

1. That the base-bed (a) is the only constant part of the Thanet
Beds.

2. That the higher and feasil hearing parts of that series (d, ¢)
occur only in the east, which partly explains why it is often
very hard to separate the Thanet Beds from the overlying series in
the eastern part of Kent, whilst the division is well-marked west-
ward; and that the unfossiliferous sand (c) thins out on the east,
so that the Thanet Beds near Canterbury may be a different thing
from the Thanet Beds between London and Rochester.

. 3. That the bottom-bed (1) is also constant, except in the far east.

4, That above this: last there is always a sand (2), a pebble-
bed (2 a), or a mottled clay (2 6), which replace one another.
toe That one very thin bed (3) in the middle of the Woolwich

* Quart. Journ. Geol. Soc., vol. xviii. p. 273.
+ See his note on the subject at p. 553.

434 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 21,

Series seems to occur right through Kent, at all events through the
eastern division.

6. That the higher and estuarme members (4, 5) of the same
series occur only in the western and central parts of the county. —

7. That the pebbles (() at the bottom of the Oldhaven Beds (ex-
cept at Upnor, where there is a little sand (a) below) are constant,
being, however, locally replaced by brown iron-ore in some places
near Canterbury.

8. That in West Kent this series lies irregularly on that below,
whilst in the greater part of Kast Kent the junction of the two shows
an accidental conformity, although the higher parts of the Woolwich
Beds are absent.

9. That it is the lowermost part of each of the three sets of beds
which is the most constant, whether from the denudation of the
higher parts, or from their more local deposition.

10. That the true basement-bed of the London Clay is also con-
stant, though but poorly represented in East Kent, and that 7ts cha-
racter depends on that of the underlying beds: thus, in Berkshire,
where the latter consist of clays and sands, it is a loam (mostly with
pebbles); on the south-east of London, in the neighbourhood of the
thick pebble-beds, it is a clayey pebble-bed ; and in Kast Kent, where
the London Clay is underlain by sand, the lowermost foot or so of
the former is sandy. |

11. That the higher divisions, the Oldhaven and the Woolwich
Series, are transgressive over the Thanet Beds, and occur as outliers
on the Chalk at or near its escarpment; so that what has been

thought to show an unconformity between the Chalk and the Ter-
tiary system would seem rather to be the result of an uncon-
formity in the lower part of the latter. To prove the existence of the
first-named unconformity it is needful that the lowest Tertiary bed,
the Thanet Series, should be present; and I think it has been shown
that where it is present (in Kent) there is as yet no stratigraphical
evidence of unconformity between it and the Chalk: paleontologi-
cally there is a break, and from the examination of a larger tract
of country we may perhaps see some signs of the unconformity
which that break leads us to expect.

EXPLANATION OF PLATE XXII.
(lilustrative of the “ Lower London Tertiaries” of Kent.)

The vertical sections in the Plate very likely do not show all the changes in
the beds; but I believe that they show the most important and the best-marked.
Full details cannot be given until various Geol. Survey Memoirs are written.

The small letters and numbers are the same as those of the respective beds in
the text.

No. 1 is made up from the many fine sections in the Canterbury and Reculvers
district.

No. 2 is meant simply to show the local thickening of the pebble-bed (8) at
Shottenden Hill. .

No. 3 is an abstract of a few sections near Sittingbourne, and has been partly
drawn with the help of my colleague Mr. Hughes.

No. 4 is a generalization of the great Upnor sections.

No. 5 is made from some road-cuttings and pits on the Cobham hills.

Quart. Journ. Geol. Soe. Vol. XXII PL XXII.

Whitaker. BA 1. Neighbourhood of
Canterbury .

5, Between Led.
& Grave.

a
—_—

Pd

.
i
|
}
|
i
{
:
|
!
:

alrite agent acti tas

LONDON Chay

OLD WAVEN BEDS

WOOLWICH AND READING BEDS

THANET BEDS

en

Sections to Utistrate a Paper “On the Lower London lerliartes of Kent” by Willvame Whitaker. BA EGS.

Diagram Section: across Tent, fron the tertiary Escarpment to the Weald. 4. Kochester

/Cpnor]
N- z &. Between Kochester

6. Plumstead Common A Gravesend.
7. Blackheath 8. &bbey Wood.

Woolwich.

3. Neighbourhood: of
Sttinghowne,

a

v0

Approximate Sea Level,

i. Lendon Gay. 2 Oldhaven Bede. 3.Woobrich Beds. +-Thanet Beds. S.Upper Chalk. 6. Lower Chalke, EU per Greensand where present.)
7. Gault. 8. Lower Greensand. 9-Weald Clay, © Siurction Tine of Thanet Beds & (halk. © Buttorn of Oldhaven Beds

z 8. Netghbourhood of
9. General Section ee ee ff

London. 1 rae

Scale of the Vertical Sections

20 Exebto are Tache

10. Genaal Section
Western Tart yh

of the ay
Londo Basin~ i

HI. The Far West
of the
London Basin.

22. What might be sean
oY de London Basin.
readied, further west.—

Engraved by TW. Lowry.

+

ve

ye

1866. ] KEENE—AUSTRALIAN CANNEL. 435

No. 6 is also made up from various sections.

No. 7 is a section of the ballast-pits at Charlton.

No. 8 is from the great brickyards at Loam Pit Hill, the beginning of the
sandy pebble-bed () being introduced from the new railway-cutting just east of
Lewisham.

The others have been drawn to show what takes place westward of Kent.

No. 9 is a generalized section from the London wells.

a No. 10 is a general section from the London Clay to the Chalk in Berkshire
¢.

No. 11 shows the westerly thinning of the London Clay and the Reading Beds,

which I have shown to bring the Bagshot Sand within 20 feet of the Chalk in

Marlborough Forest. (Quart. Journ. Geol. Soc. vol. xviii. p. 258. In the diagram

at p. 263, what are here called Oldhaven Beds are included in the Woolwich

Series, see above, p. 414.)

No. 12 is purely imaginary, being meant to show what we might see if the
London Tertiary District reached a few miles further west than it does, when,
from the thinning of the London Clay and Lower London Tertiaries, it is very
likely that the Bagshot Beds would rest at once on the Chalk.

The transverse section is simply a diagram to show the way in which the
Oldhaven beds are transgressive over those below, until at last they rest on the
Chalk, Of course this section is greatly exaggerated vertically.

Aprit 11, 1866.
The following communications were read :—

1. On the Examination of Brown Cannet, or PxErrotevm, Coat-
sEAMS at Cottey Creek, Liverpoot Prains, New SoutH WALES. ©
By W. Kauene, Esq., F.G.S., Senior Examiner of Coal-fields of

_ New South Wales.

(In a Report to Michael Fitzpatrick, -Esq., Under-Secretary for Lands, Sydney.)
[Communicated by Sir R. I. Murchison, Bart., K.C.B., F.R.S., F.G.8.]

ALREADY acquainted with the succession of deposits visible in the
various natural sections on the line and in the vicinity of the Great
North Road, so far as Aberdeen, I was desirous of working out the
geological position of the Brown Cannel Coal (specimens of which
had been sent to me from Liverpool Plains), so that I might be able
to judge of the probability of success in any search for this coal in
the district of the Lower Hunter. I therefore went to Colley Creek,
the station of Mr. Loder, and this gentleman at once offered to
- accompany me and point out the places whence he had taken speci-
mens identical in appearance with the Brown Cannel I had seen
from Hartley. |

From an examination of the rocks, I was able to determine that
the geological position of this Brown Cannel is below the coal-
seams worked in the Newcastle field—that, in fact, it forms the very
base of our Coal-measures, and in such close contact with the por-
phyries that these latter are absolutely mixed up with the lower
portion of the Cannel. I found two seams of workable thickness,
tilted at a high angle, running north and south, not far from, and
parallel to, each other, both of the same quality. ‘P

I was the more desirous of determining the geological position of

436 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr as,

this coal, because a large piece from a block of Brown Cannel was
given to me a short time ago, which had been brought up by the
buckets of the dredge working on the Hunter River, at the shallow
known as Hales’s Flat, near Morpeth. On my return to Neweastle,
and with the knowledge acquired in my examination at Colley
Creek, I went to Hales’s Flat, and had the place pointed out to me
where the dredge had been working; and it is remarkable that I
found it to be on the line of upthrow of the porphyries from the
Williams River range (which I had long ago traced across the
Hunter, near Morpeth), being the extension of the well-known Por-
phyry Point, the residence of the late Dr. Carmichael. I therefore
conclude that the piece brought up by the dredge, although a loose
biock, must belong to a deposit not far distant from the place where
it was found; and research will probably lead to the discovery of the
seam.

Geologists have defined that, of Cannel Coals, jet is an extreme
variety in one direction, as batt or carbonaceous shale is in another ;
and the specimens which I send will show you that we possess these
varieties.

I have taken the specific grayities of various specimens; and the
richness in oily products will probably be found to decrease with the
augmentation in specific gravity, the heaviest leaving the greatest
amount of solid residue after distillation. The Hartley stands first
as of the lowest specific gravity ; that from Lake Macquarie, a coarse
jet, is the heaviest (having a specific gravity of 1:5); and that from
Colley Creek shows but little difference from the famous Boghead
Coal of Scotland, of which I am also able, through the kindness of
Mr. Donaldson, to send you a specimen :—

Specific gravity of Hartley Cannel ..............sseessesseeeees 1:064
55 5 Boghead wacssvsisssac.sc tis eattt con oesankeat year 1-160
- i, Colley Creek. .iciaitsescennctemeeceenteees 1-166
35 * M)PEUCO Lich aracbanessttteeeee te rene nena 1:190
93 5 Stoney Creek ..acsisccabsasestsadesesaaseecets 1:289
hake Macquarie: «.iiicy.ccsesssive.steuecine 1:560

Chapapote or Mineral Bitumen from the Cretaceous rocks
of the soubor Wranee | ccssyeres. 1-0 antvsentartiernen tence eces 1158

Our ordinary coals vary from 1°3 to 1:4.

The small excess in the specific gravity of the dredge-specimen
over that of Colley Creek may be attributed to long contact with
water; it otherwise looks of good promise as a Petroleum Brown
Cannel, and, like that of Hartley, ignites readily in the candle-flame.

The specimens, with the exception of the Chapapote, are all true
massive Cannel Coals; and to call them ‘“ Shales” is to misname
them.

Besides Colley Creek, I heard of specimens having been picked up
in other creeks, at many distant places, particularly on the Warrah
Station; and I can have no doubt that Brown Cannel will be found
where the porphyries have tilted up the Lower Coal-measures so as
to render them accessible to the miner. The Boghead Coal of Scotland
is likewise found low down in, if not at the base of, the Carbonife-

Petit pte
Nae OT ned
a.

1866.] , KEENE—AUSTRALIAN CANNEL. 437

rous series ; for we are informed that it rests on a bed of fire-clay full
of Stigmaria, and is surmounted by shale and ironstone with plants
and shells (Anthracosia). Sir Roderick Murchison likewise states
that in the Silurian rocks of Russia there are shales yielding 25 per
cent. of bitumen and a considerable portion of inflammable gas,
and in America solid bitumen is found in the lowest fossiliferous
rocks.

T am looking for, but have as yet seen no signs of, a petroleum-
spring. In a geological report to the State of New York, on the
Seneca oil-spring the Government geologist observes, ‘“‘ There is no
necessary connexion between oil-springs and beds of coal.”

Both in proceeding to and in returning from Liverpool Plains, I
made some deviations from the road, where objects appeared to offer
matters of interest.

Rix’s Creek is the most northern colliery in work—opened by
my recommendation on my first examination of it. I descended

to the workings; and it was satisfactory to me to learn that the coal

is much approved of. In every locality as I went onwards, desires
were expressed to me that workable seams might be found; and the
Rix’s Creek Coal is actually carted as far as Aberdeen, a distance of
thirty miles. I pointed out that coal may be got near the chain of
ponds close to the railway ; and at Muswelbrook the cutting near the
town has gone through a seam of coal which, though cropping out
at a high angle, will no doubt be worked until further discoveries
are made.

At Scone, near the Kingdom Ponds, the plain is strewed with
fossil wood; and the rooted trunks of large fossil trees rising from
the ground look as though they were still in their places of growth ;
whilst a natural section in the bank of the creek or pond close by,
bordering the estate of the Honourable the Secretary for Lands,

‘shows the outcrop of the coal-seam rising from below, and regu-
larly covered by the fossil-bed.

In examining attentively the stratum of these fossil trees, I per-
Ceived signs of a marine deposit; and it became a question which of
the two was the older, the forest or the sea-bottom. ‘This was
soon solyed—a block of coral built upon and into the fossil wood

‘proved unmistakeably that the forest and the coal beneath are both

more ancient than the marine fossils covering them. This evidence,
in conjunction with that which I am obtaining from the workings at
Dalwood Creek, will set at rest the controversy as to the age of the
Carboniferous deposits of New South Wales. |
About seven miles from Scone, on the left bank of the river
Page, a limestone is worked, which I followed for a couple of miles,

to where the beds are laid bare over a large surface. I procured

Specimens, which show it to be a rich oolitic limestone. Finding it
to be encased as it were in a clay or impure limestone, I am not
without hope that some of the beds may be found to be of the pro-
portion. of clay and lime which makes cement, and I have given in-
structions for portions of these rocks to be sent to me for experiment.
I found a bed of calcareous rock near Singleton and a band of clay

438 PROCEEDINGS OF THE GROLOGICAL SOCIETY. [Apri

iron-ore of the Coal-measures below it, both beds being above the
coal worked at Rix’s Creek.

Proceeding onwards from Scone, I visited Mount Wingen, where
abundant sulphurous vapours issue from a coal-seam on fire, killing
the trees in the direction in which the wind carries the vapours ;
and, as the coal is exhausted by burning below, the ground falls in,
making fresh crevices for the exit of vapour. On the walls of these
crevices sulphurous salts are deposited, which are collected by visitors
and have much local repute for various uses.

Approaching Mount Murulla, the marine fossiliferous beds are again
abundant ; and as I heard many different stories of rocks and fossils to
be found on the mountain-top, I went to the summit, which is about
2000 feet above Murrurundi, and nearly 4000 feet above the sea-
level. For 800 feet of the ascent the mountain is flanked as by a
wall of coarse conglomerate, chiefly of quartz pebbles, in some of
which I found gold. The summit is a rough black basalt in large
angular masses, and in such disorder as to indicate violent upheaval.
The range on the opposite side of the narrow valley of Murrurundi
is of like character ; but there is sandstone in the valley, and coal is
reported to be seen cropping out in the creeks on the lower levels.
I have reason to believe that the seam which is on fire at Mount
Wingen extends into these levels, and will be found where they have
not been disturbed by eruption.

I purpose making an early examination of the deposits of Brown
Cannel at Hartley for my further instruction. Research will be
made in the Lower Hunter District for the same mineral with great
probability of suecess; and meantime the Black Cannel of Stoney
Creek, and the rich coals of Anvil Creek, and the seams of
the same group which I am successfully opening at Dalwood
Creek will probably commence to be distilled. I would also direct
attention to the Inganee seam, formerly worked at the Four-Mile
Creek, Kast Maitland, as a good Black Cannel of easy access.

There have been considerable differences in the reports of experi-
ments as to the yield in oil of one and the same coal at the hands
of different operators; but the process employed may greatly affect
the yield, and by one mode there may be driven off in gas much which
may be condensed by another. I know that it is so in the distilla-
tion of turpentine from resins; and it may be equally the case in
obtaining the products from Cannel Coal.. I would recommend that
in such experiments the gases be collected and measured as well as
the liquids, and then we shall be more correctly informed as to the
qualities of the coals experimented upon. ‘The oil in the Boghead
Coal is said to be equal to 75 per cent. of its weight. Whatever the
yield may be, the Hartley Coal is of less specific gravity than the
Boghead, and will, I have no doubt, if operated upon by the same
means, give as good results.

1866. | CLARKE—AUSTRALIAN CANNELS., 439

2. On the OccuRRENCE and GroLocicaL Position of OIL-BEARING
Deposits wx» New Sourn Watzs. By the Rev. W. B. Cuarxz,
MeA:, ¥.G.S.

[ Abridged. ]
ConTENTs. :
1. Introduction. 7. Fluviatile Drift.
2. Stony Creek. 8. Reedy Creek.
- 3. Colley Creek. 9. Colo and Grose Rivers.
4. Illawarra Shales. 10. Turon Drift.
5. River Nattai. 11. Bournda.
6. Burragorang. 12. Conclusions.

1. Introduction.—The author, after detailing the circumstances con-
nected with the discovery of Cannel Coal at Reedy Creek, at the base
of Mount York, and near the line of railway from Sydney to Bathurst,
gives a brief summary of the various divisions of the coal-bearing
beds of New South Wales; these divisions, with their estimated
maximum thicknesses, are represented in the following table :—

ie man

PERMIT A VER) BOOS fo. siuesvcraccessere bedevessorsdteeecssescaseueoes 700 to 800:
Some ENE Y, FOCKS 2 05..55 jiene oo acat Mveacles Coiaedtcoeccesecenetan 800 to 1000.
3. Upper Coal-measures (including Nattai, Wollondilly, Ila-

warra, and Lower-Hunter beds) ..............eceeseceeeees 5000.
DEE REUNIETING DOUS. .....cussonvacceacusscensivisecessecses essences 3000.
URSWEE COHI-MCASUTCS 22. ..ccccsenesesseccecucsoresesssoveenasses 1000.
6. Lower Marine beds (with as aaa abi Sigillaria, Sy-

PINGOAENATON, KC.) ...seseecveseerenrssceerensecsessseneerereees 4000.
7. Porphyry and granitic rocks rising through slates.

Further investigations will probably establish the fact that marine
fossils occur in all divisions of the above series; but it has been
already determined by indisputable evidence that, notwithstanding
the presence of Glossopteris, Phyllotheca, &c., in the Coal-measures,
both upper and lower, Paleozoic fish range up to and through the
Wianamatta beds, and are associated in great abundance with ferns
(but without Glossopteris) at the junction with the Hawkesbury
rocks, in the upper part of which the same fishes are found.

Oil-bearing products have already been found in the third and
fifth divisions. Of these, Black Cannel occurs in the latter at Stony
Creek, near Maitland, on the Hunter, Brown Cannel in the former
at Reedy Creek, and Shaly Cannel on American Creek, in Illawara,
in various creeks running into the Wollondilly and Nattai rivers, in
the Grose River, in Burralow Creek, a feeder of the latter, and in
the Colo River. The Colley-Creek cannel, which approximates to
that of Reedy Creek, I believe will also be found to belong to the
Upper Coal-measures.

2. Stony Creck.—The cannel coals and associated beds in this sec-
tion occur in the Lower Coal-measures, and are overlain by nearly
3000 feet of fossiliferous rocks, dipping at the same or a somewhat
higher angle. Gilossopteris occurs very low down in the series, which
has, by some geologists, been considered altogether of a much older
date than the formations which usually carry that genus; but Mr.

VOL, XXII.—PART I. 2H

440 PROCEEDINGS OF THE GEOLOGICAL society. _[ Apr. 11,

Daintree* has verified and confirmed the views which I have for years
been maintaining, and which have been so surprisingly combated.

The cannel from this locality has been subjected to distillation,
the produce of 180 tons of it being 400 gallons of crude oil; but
as the coke resulting from the operation is considered to be of ex-
cellent quality, it is of more value than would at first sight appear.
These beds of cannel occur again on the western side of the anti-
clinal axis, and are, it is supposed, traceable to the north bank of the
Hunter, where they also underlie the fossiliferous marine beds, eight
or nine miles to the north-east of Stony Creek ; and from below them
the lower marine beds begin to rise on the slopes of the Tangorin
Ranges. The specific gravity of this cannel varies, as does its composi-
tion; but 1:281 represents its density in a general way.

3. Colley Oreek.—On the north side of the Great Liverpool Range,
a little to the west of the 151st meridian and 80-90 miles north-
west from Stony Creek, occurs Colley Creek, in which have been
found two seams of a Brown Cannel, of somewhat higher specific gra-
vity than the black cannel of Stony Creek. Itis very like that of Reedy
Creek, but is full of grains of quartz, which give it, in places, an
arenaeous aspect. It occurs in blocks, which are superficially
decomposed into a lighter substance, but where unaltered retain a
clear dark-yellowish or light-brown hue, and split with a conchoidal
fracture, with a hard woody sound, when struck with a sharp axe or
other edge tool, the substance being tough and resisting a blow
from a round or flat tool. Mr. A. Loder, on whose estate it occurs,
sunk a shaft, and passed through a series of layers of black, partly
unctuous, clay, which appears to result from the decomposition of
basaltic rocks. A seam or mass of the cannel was passed in the midst
of these layers, which, like the cannel, contain numerous, distinct,
scarcely rounded, grains of quartz ; and these give to the clays a
porphyritic appearance, so that by sight alone one might be led to
consider them a decomposed porphyry. Between the crest of the
Liverpool Range, which is, on the Murrureaidi Pass, 2500 feet above
the sea, and Colley Creek, where the level is not more than 1600 feet,
the whole of the country consists of conglomerates and sandstones, or
of basalt and greenstone with trappean alluvial mud or clay.

The Liverpool Plains lie at a higher level than the valley of the
Hunter; and the Coal-measures on that flank of the Liverpool Range,
at about 1800 feet above the sea, are much disturbed, and also gullied
by drainage-channels. And close to the Range a considerable meta-
morphosis has occurred in the Carboniferous rocks.

It has been asserted that porphyry has intruded into these seams
of Brown Cannel ; but I confess I did not see any evidence of it ; and
I doubt whether rocks which exhibit the clearest proof of being in
part derivative from it, could be locally upheaved in the way sug-
gested. Nevertheless it is possible that porphyry may be near at hand;
yet it is very unlikely that it could have any action in saturating a
seam of coal or shale with volatile materials. It is according to ex-
perience, on the contrary, that if there be any contact between these

* ‘Geological Notes’ by R. Daintree, field-geologist, Victorian Survey.

1866. ] CLARKB—AUSTRALIAN CANNELS. 441

seams and porphyry, the volatile matter should be dispersed, and not
accumulated; and the alteration of the combustible into anthracite
or graphite would be the most probable effect*. The association of
porphyry and cannel coal is therefore merely accidental, and, so
far as my experience goes, has no bearing on the condition of the >
latter. Assuming, even, that the Colley-Creek cannel is in the
Lower Coal-measures, the arrangement is not much affected thereby,
for they rest upon and are younger than the porphyry. Supposing
heat to be necessary to produce the natural distillation required for
saturation of deposits in situ, there is no need to infer that the sup-
posed (always much exaggerated) heat of granitic rocks at the time
of eruption can have had anything to do with it. It is a fact also
that the inflammable cannels are limited in area, and oftentimes
pass off into an ordinary coal. The most that can be reasonably
conjectured on such a change is, that (supposing no objections to arise
from other principles) the volatile matters removed by distillation, or
in the change to anthracite, from one part of a seam to another part
of such a seam, have found a reception where no revolatilization could
occur. But there is no evidence to be obtained of any such transfer.
The condition of Loder’s cannel would imply that it had originally
been deposited in a marshy hollow of the Carboniferous period, to
which drift quartz and arenaceous sediment had access. The grains
of quartz are certainly entangled as they would be in a muddy or
viscid substance.

The yield of the Colley-Creek cannel is 60 gallons per ton.

4, Illawarra Shales.—Under the escarpment at the head of the
Cordeaux River and a little to the west of it,and below Mount Kemble,
in the beds intersected by American Creek, a series of shales exist
with coal, a portion of which are found to produce oil, but in incon-
siderable quantity compared with the Brown Cannels. These schist-
ose beds are arenaceous in appearance, and when taken from the
retort, after distillation, are found in lumps of charcoal, not coaked,
but with a ligneous character. They will perhaps not be esteemed
as a source of oil. With them are also schists that have a half
anthracitic or graphitic texture; and a long way below their level,
which is from 900 to 930 feet above the sea, the shales of the locally
lower coal-seams, not far above the junction with the Upper Marine
beds, are altered by basalt, which has also coked and prismatized the
coal in the Bollambi seams. Here, then, though there is some evi-
dence of oil-bearing schists, we find that character not prominent in
association with igneous rocks, but, on the contrary, the anthracitic
and graphitic characteristics are well established.

The Mlawarra Coal-measures are nearly the uppermost of the New
South Wales series of coal-bearing beds, being certainly above the
Newcastle series, and they extend for at least fifty miles, passing
upwards to the level of the Nattai or Fitz Roy beds in their exten-
sion southwards. |

Some blocks from American Creek have been taken out, which are
cut very easily with the knive, leaving a clay-like surface, and hav-

* See Delesse, Métamorphisme des roches, pp. 305-314.
De,

442 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apri.

ing the usual woody sound when struck. They ignite readily by a
lighted match. The section exhibits an escarpment of 500 feet of
Hawkesbury rocks resting on 800 feet of Coal-measures, which exhibit
various distinguishing differences when compared with the Newcastle
beds, and are supported by the Upper Marine beds, which rise in a
dome-like form, and exhibit an approach rather to the beds immedi-
ately below the Muree series than to those of that place, reminding
one of the deposits near Harper’s Hill, where basalt, as in the neigh-
bourhood of Wollongong, intrudes into and disturbs them, and where
they are succeeded by just such beds as mark the base of the Coal-
measures under Mount Keira. Certainly the Newcastle coal-seams
are not represented in the Illawarra section; but the evidence is
perfectly distinct as to the inflammable beds belonging to the upper
part of the Upper Coal-measures.

A view has been taken by some observers, of the connexion of the
Ilawarra and Lower Hunter coal-beds, which would place them in
the same angular relation with the axis of the basin. This I believe
to be altogether erroneous. A considerable portion of the eastern
side of it has been entirely swept away; and traces of former surfaces
which must have belonged to a wider area are now apparent on the
summit of insulated points along the coast, that can only be accounted
for by admitting the destruction of considerable masses. This ex-
planation was offered by myself many years ago, and has been con-
firmed by more recent observations. Others have adopted this opinion ;
but they have not coupled it with the fact, which I consider capable of
clear establishment, that the Illawarra and Newcastle beds are not
in the same plane. The coast-line is not that of the axis of the
basin, but cuts it obliquely; so that different portions of the same
series of beds are represented in what would otherwise be about the
same longitudinal horizon. Looking at the matter in this way, the
strike of the Illawarra beds would appear to be full 25 miles to the
eastward of Newcastle, which will account for the existence of beds
in the former district which are not represented in the latter, but
which were once continuous over them. A further deduction from
this view is, that parts of the Coal-measures of the Illawarra, the
Shoalhaven, the Wollondilly, and the Cox river-basins are unques-
tionably the uppermost portions of the great eastern coal-field, the
middle and lower parts of which are so abundantly developed in the
basins of the Page, Goulbourn, and Hunter river-basins.

Were it possible here to enter into a close investigation of this
subject, by reference to the evidence of the fossils collected from
the different members of the series, it could be shown that the cha-
racteristic species of the upper beds are not altogether those of the
middle and lower, although, generally speaking, there are the same
genera in all.

5. River Nattaa—The Upper Coal-measures extend along the
heads of the creeks forming the Nattai River; these creeks run in
deep ravines, cutting the series from the Hawkesbury rocks down to
the Upper Marine beds, which come in (as at the same distance in
the Illawarra,ascending Mount Keira) about 250 feet below the lowest

1866. | CLARKB—AUSIRALIAN CANNELS. 443

coal-seams. The Coal-measures thence range to the southward as far
as the banks of the Shoalhaven and Wollondilly rivers, the older or
Hunter-River beds cropping out from under the upper. About the
heads of the Nattai the whole series has been disturbed by the in-
trusion of igneous rocks in the Mittagong (or, rather, Merrigang)
Range. Immediately upon the older trachytic diorite of the ex-
tremity of the range, where it attains an elevation of nearly 2800
feet, at Bourell or Gibraltar Gap, but altered by more recent basalt,
repose the fragmentary patches of the Hawkesbury rocks, covered by
the Wianamatta black shales, in which are a profusion of stems and
leaves of Phyllotheca, Cyclopteris, Sphenopteris, and a new genus
having the venation of Diplazites, together with the following generic
forms of fish :—Myriolepis, Cleithrolepis, Palconiscus, and one or two
others.

The shales which contain these fishes are precisely those of the
fish-beds of Campbelltown, which also occur at the junction of the
Wianamatta and Hawkesbury rocks.

The insulated hills in advance of the Merrigang form the fine
Mittagong of the aborigines. One of these summits slopes down to
the iron-mine to the south, and, at an elevation of 570 feet above the
working coal-seam at its base, forms the top of a precipitous escarp-
ment to the north, at the base of which occur four seams of coal, from
some of the shales of which I procured Glossopteris and M‘Coy’s new
genus Gangemopteris. In the ravines to the north-west, about three
miles from Fitz Roy, the seam was found to have thickened to 38 feet
64 inches, and appears to have below it a bed of basaltic greenstone
(one of the intrusive dykes of the igneous outburst which exerts so
extensive an influence for many miles round Mittagong); and from
250 to 300 feet below all the Coal-measures there occur marine beds
with Trochus, Spirifera, &c.

Above the great seam and at the base of Mittagong is a Cannel-
coal. |

The Coal-measures of this neighbourhood are treated of because they
belong to the upper measures, and contain peculiar beds, which
again present themselves on the Wollondilly, where blocks of brown
oil-producing Cannel have been found. Silicates of alumina, and
coals full of small cavernous spots (the latter often filled with
hydrated oxide of iron in the form of seeds), mark some peculiarities
of these deposits ; and these again occur in Burragorang, and occa-
sionally further to the west, about the sources of the Cox.

6. Burragorang.—This is a local name for the part of the Wollon-
dilly valley which occurs between the junctions of the Nattai and the
Cox with the former river, and the section of which shows completely
that the order of deposits is similar to that of the Iawarra and Nattai.
The Upper Marine beds, which occupy the bottom of the section, agree
in part with those of Maree, near the junction of the Williams and
Hunter rivers, passing into the next lower set of beds in that
neighbourhood; they support a series of coal-measures which are
capped by Hawkesbury rocks, all resting apparently in a nearly

444 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apro ie

horizontal position on each other. At the junction of the Nattai the
lowest beds are seen dipping only slightly to the westward.

Near the junction of Toonalli River a dry creek intersects the beds
of a spur from Toonalli Mountain, locally called “The Peak of
Teneriffe.” In this creek I found in undisturbed position white
and blue shales with Glossopteris. The bottom and sides of the
creek are encumbered with fallen blocks from the upper quartzose
sandstones and intermediate beds of similar kind below the Hawkes-
bury beds; and amidst these blocks occur also others of inflam-
mable shale passing into Brown Cannel. The seam was ascertained
to lie between 900 and 1200 feet above the sea, and consequently
is not far from the base of the Hawkesbury rocks. There are on
the flat at the base of the spur several water-worn blocks of this
Cannel lying on the surface of the ploughed ground, which rests
upon a red and yellow grit of the Upper Marine beds. These are
about 9 inches thick, whereas up the creek the blocks reach a
thickness of 12 or 14 inches. Only one conclusion ean be drawn
as to the blocks upon the flat—namely, that they have been drifted
by floods to their present position. It is quite impossible that
they could occur actually bedded as a coal-seam with the marine
beds without any accompanying shales or clays; and it is equally
impossible that they can belong to one seam highly inclined, for
the beds have a dip, if any, in a contrary direction to the implied
upheaval.

Nearly opposite the mouth of the Nattai, the Upper Marine for-
mation attains an elevation of 500 feet above the valley, so that
the three successive groups of beds have nearly equal vertical
dimensions. In a recess of the ranges near the head of Lacy’s
Creek, the Middle or Coal-measure series is generally plainly exposed.
The junction of the latter with the Hawkesbury rocks is marked ~
by springs, and the regular stratification of the beds both above
and below this junction is remarkable ; their fall is about 100 feet
in succession, until the white shales are reached, where a similar
concealment to that on the Tonalli River takes place, from detached
huge blocks of coarse grits and sandstones.

A coal-seam, extremely like one of the Nattai seams, has strewn
its fragments on the ledge below the springs; and blue shales and
mottled clays mark its position somewhat higher up. The blocks
that obscure the beds originate in a system of three-jointed planes
cutting up the beds, which are thus rendered capable of supplying
materials for a débacle.

7. Fluviatile Drift.—The river-bed and bottom of the Wollondilly
valley, for a depth of 40 feet and upwards, is covered by a fluvi-
atile drift of hard pebbles, chiefly porphyritic, with very little
granite, (probably because it easily disintegrates), some sandstone,
and coal mingled with sand. This drift I have traced along the
Warragamba, and the shoulders of the ridges above it, into the
‘Wianamatta, region, across the latter in directions corresponding
with the Wollondilly and Goose, to Emu and Penrith, and across

1866. | CLARKE—AUSTRALIAN CANNELS, 445

the country to Windsor, Wilberforce, and to the river Hawkesbury,
where, at a distance of forty miles from its river-sources, this
drift is found in solitary pebbles.

At Penrith there is an accumulation of them to the depth of
several feet on the river-bank. Emu Plains and the bed of the
Hawkesbury are covered by them (and Lapstone Hill takes its name
from their presence) as high up as 400 feet.

At Cox’s basin, where the Warragamba joins the Nepean, there
is also an island formed of drift, in which porphyry, hardened sand-
stones, and coal occur. But it is remarkable that there is in these
accumulations very little, if any, granitic rock besides porphyry, and
no basalt or other trap; whilst in the trappean ash which occurs at
Cox’s basin and in the Kowmery River, a feeder of Cox’s River, por-
phyry and bastard granite are imbedded.

Nothing can so clearly mark the origin of the deep ravines by
continual washings and erosions (probably after some dynamical
action had fissured the country) as the fallen blocks of the plateau,
and the pebbles which cover the surface of the country in the line
of drainage.

8. Reedy Creek.—On the eastern arm of the fork at Mount York,
which is now called Mount Dixon, there exists a bed of very rich
iron-ore; and iron also occurs near the head of the Reedy-Creek
valley, which extends to the west. Below the ironstone occur sand-
- stones, shales, and coal-beds ; but at the level of the valley the Cannel
stretches across it, and when I first visited it seemed to consist of
blocks of from 6 to 12 inches thick. Now that the seam has been
opened and worked into the boundary ranges, it is found much
thicker than was anticipated.

The section is as follows :— faepmanahan!
Nines GNA ee tk ed cwrart as pare tinge fis oh ae eee ainda shies 0 :
SUTLON giles SN ES RINE sie BPE SIG ae RRR Oe EN ere 1
Rune lam@ ariel "ert cians ce cers tet isso ae cateelaitteeinieion cectare ae eee eae 4 0
@anmnel Coal, less rich! As.2 8s .c enlace ose enesess ences 0 6
5 9

The Cannel dips about east by north at from 1° to 2°, or about 1
in 35; in places it is full of fronds of Gilossopteris, and a plant
branching after the manner of Asterophyllites, which lies in perfect
unrumpled order; it also puts on a prismatic structure, and has
a flat but well-marked conchoidal fracture. The shales are im-
pressed with Vertebraria, Glossopteris, and Gangemopteris (M‘Coy).
The Cannel passes into true bituminous coal in parts of its course ;
and the shales in contact are earthy, but very inflammable. The
toughness is remarkable. The produce of the rich Cannel is from
150 to 160 gallons of oil (realizing 100 gallons of pure oil) and from
1700 to 1800 cubic feet of gas to the ton. This seam appears, by
borings commenced in the vicinity of Mount Victoria and to the east
of the first workings, to be extremely variable in dimensions and
composition. At the Sugar-Loaf, part of the Mount Victoria range,
a seam was pierced re is but 2 feet thick. It is supposed to re-

446 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 11,

present the Reedy-Creek seam ; but as it is 300 feet or so above that
level, it would rather belong to the coal-seam at the height of 3000
feet on Mount York. A further discovery of Cannel, but not so rich
as the original, has been made south of the foot of Mount Victoria,
in two spots where the Cannel proved to be from 15 to 18 inches and
21 inches thick respectively. It is, so far as is at present known,
quite clear that these seams are in patches, and not of uniform thick-
ness; and consequently it would be premature to build expectations
of any kind as to the extent in space occupied by them.

9. Colo and Grose Rivers.—The existence of Cannel of the Reedy-
Creek kind is not altogether confined to the western side of the pla-
teau ; for in the Colo River and in the Grose also, and in the Burralow
Creek, which flows to the latter from the Kurrajong, rounded pebbles
of Brown Cannel have been found, as I learn from my field-notes
made many years ago, and from specimens more recently collected.

Both the Colo and Grose flow through gorges and ravines like
those of the Nattai and Wollondilly, but not so accessible as the
latter. As there are considerable deposits of coal about Wolgan,
Capertu, and Cherry-tree Hill, where there is a seam 10 feet thick,
it is not improbable that the Colo-drift Cannel may haye come down
from the higher parts of the river.

In the places mentioned above, the same genera and species of
plants which occur in the Coal-measures of the Nattai and Wollon-
dilly are also found; and these same fossils are abundant in the
shales at the head of the Turon, and also at the head of the Cox,
and under Hassan’s Walls and Mount Clarence; so that the Upper
Coal-measures are everywhere distinguished in the area under review.

It is quite clear, therefore, that the Orl-bearing shales and Can-
nels are, in the eastern Coalfield of New South Wales, entirely con-
jined to the upper group.

10. Turon Drift.—About Bowerfells, and at Brucedale, on the
Winburndale rivulet (near Bathurst), there is a drift of another kind
from that of the rivers over the Wianamatta beds. It consists of frag-
ments,much rounded, of yellow sandstone, full of Spirtfera, Orthis, &e.
It was not until very recently that I ascertained the source of these
fragments. Some distance below the head of the Turon River there
is a place called the Gun, which is surrounded by ranges fully 1000
feet high; the bottom of the gulf is formed of slates, from which
the gold of Sofala has been derived; and over them occurs a ferru-
ginous conglomerate, which is succeeded by thick beds of the Bra-
chiopod-sandstone, over which come in conglomerates, shales, sand-
stones, and the coal of Cherry-tree Hill, surmounted by the Hawkes-
bury rocks. In the drift of the Turon, about Sofala, occur blocks
of hardened sandstone impressed with Lepidodendron.

In like manner the Brachiopod-bearing sandstone is strewn
about in the river-drift of the Moruya to the southward, from
which it is to be inferred that the whole of the groups connected
with the Carboniferous formation have been broken up and dis-
persed. Where, however, the Hawkesbury rocks cover them, the
Upper Coal-measures are in some degree protected.

The success which appears to have attended the working of the

1866. ] ‘CLARKE—AUSTRALIAN CANNELS. 447

Reedy-Creek Cannel has excited so much interest that all kinds of
substances have been forwarded for examination, and among them
black clays from various parts of Manearo, some of which, on
analysis, have shown the propertion of ash to volatile and carbo-
naceous matters to be as 77 to 23.

11. Bournda.—There is, however, another kind of deposit which
demands notice.

The coast, for many miles to the northward of Cape Howe, is
formed of rocks which belong to the Lower Silurian formation,
and consist principally of purple schists with quartz veins and
with some beds of purple slate and sandstones. Along the shore,
as just north of Eden, at Pambula and Meribula, beach-lakes
occur, and some of those further to the northward are partly
blocked by sand. At Bournda there is a tract of country in which
formerly a lake or lagoon existed. It is now not altogether dry ;
and though not much timber exists there, there is a considerable
growth, on the dried surface, of that peculiar vegetation which
clings to a soil made up of sand and marsh. The coast-line inter-
sects the deposits which form the base of this tract, and which
rest upon the highly inclined purple slates, granite occurring at no
great distance. The age of the deposits is probably of the recent period.
There is no evidence of any Tertiary epoch; yetit has some resem-
blance to a Brown Coal deposit.

A section of 60 feet of the cliff at Bournda gives the following
succession of deposits:— —

1. White decomposed granite full of rounded bits of quartz like that of
ranite.

‘i 2. Rather more yellowish decomposed granite, of like kind, with roots of
recent plants.

3. Very gritty pale deposit with woody matter.

4. Yellowish, and occasionally reddish, sand (in the condition of dune sand),
with partly abraded particles of quartz.

5. Greyish-white clay, strongly adherent to the tongue, with recent plant-
fragments.

6. White, fine, friable, very slightly gritty clay of a kaolin character, pro-
bably useful for fire-clay and pottery.

_ 7. Blackish muddy laminated deposit, full of vegetable patches, much iron-
pyrites, and some lignite.

8. Dark yellowish-brown laminated deposit, 1 foot thick—the ‘ Bournda”
so-called “ lignite,” being a clay-bed saturated with volatile matters, resting on—

9. A partly reddish, partly brown, sandy and earthy deposit, with an abun-
dance of small quartz pebbles.

The lower part of the deposit has been entered to the extent of
fifteen yards; itis found to be four feet thick, and has been sub-
jected to chemical analysis. It seems to have been a mud satu-

rated with oily ingredients, and is highly inflammable. It is not
altogether a true peat, but may be regarded as such, having
probably had a similar origin and afterwards been covered by
flood-detritus brought down from the ranges. None of the sand-
or clay-deposits exhibit any evidence of calcareous matter; the
explanation, therefore, of its lacustrine origin on the land is pro-
bably the correct one.

A year ago I received from a creek about forty miles north of

448 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 11,

Bournda a white waxy mineral, which comes very near “ Bog But-
ter” in appearance and chemical composition. Probably this was
a peaty product, and, as such, is in correspondence with the Bournda
deposit, to which latter it is difficult to assign either the name of peat
or lignite. I have called it “ bog stuff.”

The following results of distillation assign its actual character :—

lay AT SANG os pene cecnen: aeons 15°60

Residue’... /....0s.-0- Other inorganic matter ......... 0:68

GATOOM IRE eek coe rade ates 8°75

Gaga Water 4 Er Oe Pea 48:00

Volatile Products q i e= 0c De ne ees 8:00
(ASP OUG eaves Meopiewsieiehloce seniee 19-00-———_100-03

The tar-oil is butter-like and viscid, but it contains a proportion
of what is called solar oil, lubricating oil, and paraffin, to the amount
of 35 per cent.

The gas was at first bluish at low temperatures, but became after-
wards white, and very offensive from sulphuretted and phosphor-
etted hydrogen.

It may be suggested that, mixed with the better-class coal of
New South Wales, it is likely to be valuable for the production of
gas. It has been ascertained by actual experiment that three tons
of this Bournda deposit are equal, in the manufacture of sulphuric
acid, to two tons of coke.

12. Conclusions.—The chief conclusions arrived at are :—

1. That, with the exception of the Stony Creek Cannel, all the
oil-producing deposits occur in the Upper Coal-measures ; and that
the Cannel of Stony Creek, on the river Hunter, occurs in the
Lower Coal-measures, which are above the Lower Marine beds with
Trilobites, below which, again, are numerous fossiliferous beds before
the porphyry is reached.

2. That the Cannel belongs to beds in which Glossopteris occurs,
and therefore may be a slight additional evidence of their antiquity,
as it is an analogue of the “‘ Bog Head” Cannel of Scotland.

3. Remarks on the CoppER-Minzs of the Stats of Micutean.
By Hitary Bavrruan, Esq., F.G.S.

ConrENTS.
1. Introduction. 6. Mines of the Northern District.
2, Structure. 7. Ontonagon District.

3. Metallic Minerals of the District. | 8. Paragenesis.
4, Mode of Occurrence of the Copper. | 9. Origin of the Copper.
5. Distribution and Association of the

Copper.

1. Introduction.—-The remarks contained in the following pages are
the results of a general examination of the mines of Keweenau Point,
made during the summer of 1865; and although the subject is not a
new one, having been elaborately treated by Professor Whitney in two
different works, and having received subsequent notices from Messrs.
Rivot, Borie, and others, still the progress of mining enterprise has

1866. ] BAUERMAN—COPPER-MINES OF MICHIGAN. 449

opened up some new features which have not as yet received any
notice, and may be of interest to the Society.

The copper-mining district of Michigan is situated in the upper
peninsula, or north-western portion of that State, forming a nar-
row belt of country about 140 miles in length, extending in a
north-easterly and easterly direction, from the boundary of the State
of Wisconsin to the end of Keweenau Point, the promontory of
which projects into Lake Superior on the southern shore, about mid-
way between Fond du Lac and the outlet of the lake at Sault S.
Marie.

2. Structure of the District—The rocks of the district consist of
coarse sandstones and conglomerates, occupying either shore, witha
central mass of trappean rocks, which forms the mineral range proper.
The sandstones on the eastern side have a south-easterly dip, while the
traps, which are well stratified, and include several conformable beds —
of conglomerate, together with the overlying sandstones and conglo-
merates of the western and northern shores of Keweenau Point, dip
towards the north and north-west, or generally at right angles to
the trend of the land.

The surface of the country is for the most part covered with a
dense forest, interspersed with smail lakes and swamps. In the
drier ground maple is the prevailing timber, with spruce, pine, and
oak, in less quantity. Cedar is common in the swamps, which are
also remarkable for their profuse growth of enormous plants of
Osmunda cinnamomea and other large ferns characteristic of wet
ground.

In the northern district, and as far west as Eagle River,
the rocks are free from cover, the sandstones and conglome-
rates on the north shore forming a steeply-scarped cliff, sur-
mounted by gently sloping inclines on the upper surface of the
beds. At Copper Harbour the face of the escarpment of one of
the conglomerates is so very regular that, owing to the wood
having been burnt off, it may be traced, forming a perfect wall
without break, for several miles. Further to the westward, however,
the geology becomes very obscure on account of the drift, which ex-
tends from near Kagle River to the extreme point of the district
beyond the Ontonagon, and, in greater or less thickness, effectively
covers up the rocks below. This drift is composed of a stiff blue or
reddish clay, passing up into sands or gravels, and in places is full
of angular or scratched stones. It is of great thickness in some
places—as, for instance, at the Naumkey mine, on the south side of
Portage lake, where a shaft was abandoned from excessive influx of
water, after 100 feet of sand had been sunk through without reach-
ing the rock. Sections of contorted drift are seen in considerable num-
bers in the drift plateau which forms the belt of country below the
Minnesota hills and the lake-shore near Ontonagon. The surfaces
of the rocks immediately below the drift are often scored and striated
by ice, the furrows being sometimes of extraordinary size—for in-
stance, at the Concord mine, on Portage Lake, where they are nearly
semicircular and about 14 inch deep. The general direction of

450 PROCEEDINGS OF THE GEOLOGICAL socieTy. [Apr. 11,

the glacial striations is about north and south ; and the drift occasion-
ally contains Upper Silurian fossils, which have been derived from
the country between the north shore of Lake Superior and Hudson’s
Bay.

From the preceding remarks on the nature of the surface, 1t may
be understood that the order of sequence of the rocks is notas yet quite
conclusively determined, and that therefore there may be some doubt
as to the proper age to be assigned to them, fossils being absent on
Keweenau Point. Where the rocks are bare, the section has been
well made from shore to shore by Mr. W. H. Stevens; and they are
shown to be in conformable sequence from east to west. At Portage
Lake the lower boundary of the trap is hidden; and, indeed, researches
subsequent to those of Messrs. Foster and Whitney have shown
that more ground is included within the trappean range than is laid
down on their map. In the original survey of Messrs. Foster and
Whitney, these beds were assigned to the Potsdam or Lowest Silurian
group ; but subsequent investigations have led Prof. Hall and Sir
W. E. Logan to refer them to a somewhat higher level, or in the
Quebec group—the former geologist having determined that the
mass of the sandstones of thé Sault 8. Marie and the south-eastern
shore of the lake are equivalent to the Saint Peter’s sandstones of
Minnesota, forming probably part of the Chazy formation*. On the
Canadian side of the lake, the traps are penetrated by intrusive
dykes which do not affect the overlying sandstones; but there is no
good evidence of asimilar unconformity inthe upper beds of Keweenau
Point, as no transverse dykes are seen. I have examined the junction
of the traps and sandstones at three different points—namely, at Port-
age Lake, Copper Harbour, and Eagle River. In the latter case the
junction-surface was perfectly smooth, without any indication of
intrusion ; while in the two former afew small irregular veins, filled
with a red jaspery substance, are given off from the traps, and
penetrate the sandstones and conglomerates to the depth of a few
inches; but this evidence is too inconsiderable to have much weight,
in view of the abundant proofs of conformable stratification derived
from the regular alternation of the conglomerates with the igneous
rocks.

The central trappean belt, forming the mineral range proper,
varies in width from 2 to 3 miles, and extends throughout the
whole length of 140 miles, passing into the neighbouring State of
Wisconsin. The prevailing rock is mineralogically a dolerite, or
mixture of felspar (labradorite), hornblende, and augite, with chlorite,
epidote, calcite, and magnetite as occasional constituents. It is
usually of a dark-brownish-red or chocolate colour, mottled with
green or black by the chloritic material, but occasionally becomes
bright green, or even sulphur-yellow when epidote prevails, as is
the case in the Ontonagon district.

. More important, however, than the mineralogical constitution of
the traps is their physical structure, which varies considerably, the
commonest condition being compact, with finely granular fracture,

* Geology of Canada, pp. 84-85, Atlas, p. 19.

1866. | BAUERMAN—COPPER-MINES OF MICHIGAN. 451

with only a few small empty vesicles, the joints being irregularly
disposed, giving fragments of no defined forms. Near Eagle Har-
bour a well-marked columnar bed is seen, which has been traced for
several miles. Another more important bed of a crystalline character
occurs a little lower down. This is the so-called “ greenstone,” a
finely crystalline rock without ‘vesicles, which appears to be nearly
homogeneous, and of a dark green colour on a freshly fractured
surface; but a concretionary structure is brought out by weathering,
the exposed surface presenting a finely mammillated appearance,
The thickness of this bed is from 500 to 800 feet, according to.
Whitney ; ; and where present in force it forms a well- marked feature
in the scenery, the escarpment being in fact the “ chiff” after which
the oldest and most successful of Lake Superior mines isnamed. It
has been traced from the Point eastward for about 40 miles, and is
used to divide the mass of the trap into the northern and southern
ranges—a distinction that cannot be established in the Portage Lake
district, where the greenstone is absent, or covered up with drift.

Scattered through the massive trap are beds of amygdaloidal
character, containing cavities that have been subsequently filled, by
infiltration, with foreign minerals, usually zeolite and calespar, with
chlorite, epidote, and native copper in the mineral range; whereas
chaleedonic amygdules, agates, and similar siliceous substances
characterize the amygdaloids of the higher or Lake-shore traps at
Eagle Harbour, Copper Harbour, and Agate Harbour, &c.
3. Metallie Minerals of the District.—In addition to the native metal,
other copper-bearing minerals have been observed, but only in small
quantity: these include a rare substance called Whitneyite (which
is the most basic of the known components of copper and
arsenic, its composition being represented by the formula, Cu 18, As,
with 88:36 per cent. of copper, and 11:64 per cent. of arsenic),
copper glance, and the various oxidized ores, such as chryso-
eolla, malachite, azurite, cuprite, and melaconite. The latter mi-
neral, although not of present importance, is of interest as having
laid the foundation of mining industry in the country, the first ope-
rations of the Cliff Company in 1847 having been upon a vein in the
upper conglomerates of Copper Harbour, which produced about 25
tons of mixed silicates and black oxide of copper, being the only
instance in which a deposit of any extent has been found in the top
beds. Copper glance has been found in small quantities in a vein
at the Huron mine on Portage Lake, and more abundantly at the
Mendola mine near Lac la Belle, in the lower or southern portion of
the mineral range, which is now being explored in a regular manner.
The arsenide occurs in a quartz vein at the Shelden Columbian mine,
and in an unworked deposit on the Lexington location south of
Portage Lake, where it has been got in masses of several hundred-
weights. This mineral, although rare, is of interest, asit also occurs
in the copper-mines of Chili.

4. Mode of Occurrence of the Copper.—In addition to its presence
in the amygdaloids, copper is found in one of the conglomerates
associated with the trap rocks, finely interspersed in the more epi-

452 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Apr. 11,

dotic portions of the latter, and in two classes
of true lodes,—one of which crosses the strata at
right angles to their strike, forming the so-called
fissure-veins of the Keweenau Point and Hagle
River districts ; while the other includes such
velns as run with the formation, and are found
in the Ontonagon district. These are very irre-
gular in character; and the fact of their being
veins can only be made out by their relations to
the containing rocks as developed in deep work-
ing, the surface appearance being that of irre-
gular masses of epidote-breccia, continually
varying in thickness, although capable of being
traced for considerable distances. In the fissure-
veins the metal occurs in comparatively smooth
platy masses, of all sizes, and comparatively free
from intermixed rock; while in the Ontonagon
lodes the masses are rough and on a very large
scale, arborescent in form, and usually contain
large adherent and included fragments of the
vein-stone—a breccia of epidotic rock and
quartz; but in either case they may attain a
great size, and at times a weight of several
hundred tons. In the cupriferous amygdaloids
of Portage Lake, masses of great size are not
found, the largest being that discovered about
two years since in the Mesnard location, which
weighed about 18 tons, and lay loose on the
| aN drift covering the rock. In addition to the

SN masses, thin sheets of metal are common wherever
narrow transverse cracks occur in the rock,
either forming masses of tangled crystals with
a serrated edge, or, when of large size, being
more compact and not unlike worn-out copper
sheathing. The metallic kernels of the amyg-
daloids are rarely solid, but form thin shells
moulded to the wall of the cavity, or to the
crystals of some mineral previously deposited,
usually carbonate of lime. In the conglome-
rates, in like manner, the metal usually incrusts
the pebbles, sometimes completely investing,
but never entirely replacing them. When cry-
stallized in its own form, the copper has also a
great tendency to appear in hollow crystals, the
simplest solid forms being formed in the hol-
lows of the larger masses. A fine example of
this has been recently furnished by the great
mass of the central mine, which on one of the
cuts disclosed a druse full of nearly perfect
crystals of tetrahedral form, without any se-

BR. 30° 8.
Sand stones.

Mabb’s Lode.

Isle Royale Series.

ASS

Pewabic Series.

Fig. 1.—Section of the Trappean Belt of the Mineral Range.

Hancock Series.

Sandstones and
Conglomerates.

1866.) — BAUERMAN-——COPPER-MINES OF MICHIGAN. 453

condary planes. The finest crystallized varieties are, as a rule, ob-
tained from the Ontonagon district, and generally are more abundant
in newly opened mines than in those which are worked at greater
depths.

In the Porcupine Mountains, to the west of the Ontonagon River,
a compact epidote rock is found containing copper in such a very
finely divided state, that it has hitherto been impossible to work it
advantageously. Native silver is found to a small extent, either
erystallized in arborescent forms, or irregularly spotted through the
copper, the line of separation between the two metals being well
marked in polished specimens. The Cliff and Minnesota mines have
produced the largest amount of the precious metal, the absolute
production, however, being but small; and scarcely any portion of
what is found comes into the hands of the mining adventurers,
except a few pounds which are annually got by hard picking from
the coarser sizes of the dressed mineral. The larger pieces find their
way into the hands of dealers and collectors, the earlier miners
having appropriated them to their own use, and the precedent has
been persistently followed ever since.

5. Distribution and Association of the Copper.—Among the three
classes of deposits in which the mines are worked, the most important
are the stratified amygdaloids, which will therefore be first considered:
They are confined to the district of which Portage Lake (an inlet
which nearly cuts the Peninsula into two parts) is the centre. The
oldest mines are on the southern or Houghton side of the lake, so
called from the town or village named after the geologist who
examined the country; while the newer and more important ones
are on the northern side, above the village of Hancock. The banks
of the lake on either side rise steeply from the water to a height of
from 400 to 600 feet; the dressing-flows, being placed close to the
water, receive the ores from the mines (which are located on the high
tablelands above) by means of railways and inclined planes. Taking
the extreme north and south mines as limits, the district has a
length, measured along the strike of the trappean belt, of about 9
miles, and a breadth of from 3 to 5 miles. The general section,
showing the position of the copper-bearing beds, is as shown in
Fig. 1. The series of beds indicated are amygdalous traps, which con-
tain more or less copper in the cavities, and are regularly mined under

_ Fig. 2.—Section from the Pewabie Lode to the Albany and
Boston Conglomerate (530 feet).

2 > 8
2 ; Albany& OO» . aa p
' Pewabic Lode, Old Pewabic Green Amygdaloid Boston a a oe]
12 ft. Lode, 32 ft. Lode, 19 ft. Lode, 7ft. 9% 542
i .

= “fs ip
a) Oy 7 DAS, by fv ff 2
Lig SED. he

the name of “lodes.” In the uppermost or Hancock series, only
one mine 1s opened, bearing the same name. The ground is more

454 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Ape

irregular than is usual in the lower beds, three different belts of
metalliferous rock being known. ‘The principal one is 24 feet thick,
without any defined walls; and about one-half of it is workable: the
drivage is done on the upper or hanging wall, which often presents
a laminated appearance from the occurrence of strings of calespar,
testing cross-cuts being driven into the vein below at intervals; the
copper mass is chiefly on the lower or foot-wall side, the upper part
being a hard compact trap. The yield of the rock sent to the stamps
in 1864 was about 272 lbs. per cubic fathom, equal to 15 lbs. per
ton, or about 2 per cent.

The second or Pewabic group is more important than the preceding,
and includes several belts.or lodes, whose thicknesses and positions
are given in Fig. 2, which represents the section obtained in a cross
cut made at the 70 fathom-level of the Pewabic mine.

The most important members of this series are the highest, or
Pewabic lode, and the lowest, or Albany and Boston conglomerate.
The former has been systematically mined by the Quincy, Pewabic
and Franklin Companies for a length of about 13 mile in a north-
easterly direction from the Hancock shore of the lake. North of
the Franklin it has been traced, but not worked, for a further length
of about 33 miles, up to the Albany and Boston mine. It is a dark
brownish-red amygdaloid, filled with small vesicles containing
chlorite and native copper; the thickness varies from 6 to 30 feet,
the average being 9 feet in the Pewabic, and 10 feet in the Quincy
mine; the hanging wall is a compact greenstone-like trap; while

4 , . the foot-wall is adark-coloured amyg-
DE OUR daloid, withvery small kernels of oa

EOE ee Fig. 3 shows the character of
fm. level, Pewabie Mine. the Jode at the 130-fathom level of the
Pewabic mine. Copper is well sprin-
kled through the whole mass, with a
few small masses near the foot-wall,
and with irregular calespar strings in
the upper side. Although not produ-
cing any very large masses, the yield is
tolerably uniform, the produce being
at the rate of 1-5 per cent. in the
Pewabic, and 1:6 per cent. in the Quincy mine: the latter is sunk
below the 100-fathom level. The concentration of the copper
towards the foot-wall is characteristic of the whole of the amyg-
daloids.

The other members of the group, below the Pewabic lode, although
not of any great importance as regards produce of copper, are of
interest as establishing the regular succession of the amygdaloids
over areas of a certain extent, the section being substantially the
same in the Pewabic cross cut as it is in the Albany and Boston line
about 33 miles further north. It is not necessary to go further ito
the characteristics of these belts or lodes ; but it may be incidentally
remarked that the epidote lode is filled with a purplish rock, contain-
ing a great deal of bright-green epidote, and that the Albany and

1866. ] BAUERMAN—COPPER-MINES OF MICHIGAN. 455

Boston lode is also very epidotic, and in the hollows carries large
quartz crystals and masses of prehnite.

The Albany and Boston conglomerate is a deposit of considerable
interest, as it forms a well-marked horizon in the rocks of the
Portage distriet, and carries in places a very considerable amount of
copper. It is about 30 or 32 feet in thickness, and is ineluded
between a soft argillaceous sandstone floor, 4 feet thick, and a clay
roof of 9 inches in thickness. The latter contains at times parallel
sheets of copper, and is locally known as the “flucan lode.” The
pebbles are chiefly of red jaspideous porphyry, and are for the most
part well-rounded, varying in size from about half an inch up to six
or eight inches in greatest diameter. The cementing material varies
considerably, being mainly calcareous at the Pewabic, and a compact
epidote at Rhode Island mine. The more usual character, however,
is a granular mixture of epidote, quartz, and finely divided rock-
matter with small specks of copper.

More remarkable conditions, however, have been observed in some
portions of this rock at the Albany and Boston mime, where the
cement is in places entirely metallic, the copper forming elosely-
fitting shells over the pebbles, and at times permeating them to such
an extent as to form, with the siliceous mass, a kind of eopper-con-
erete, which of course is extraordinarily tough, such pebbles being
eapable of passing almost unaltered in form through the jaws of the
powerful rock-breakers employed in the dressing-floors. In places,
however, the copper in the cement of the coarse conglomerate has
been changed to chrysocolla and red copper ore, both of the octahedral
and fibrous forms, associated with which are calcspar, prehnite, and,
probably, cupreous allophane. Out of the total thickness of 32 feet,
only the lower portion of the bed, from 10 to 15 feet in thickness, is
eupriferous ; so that in this respect the conglomerate resembles the
amygdaloids.

The lower metalhferous, or Isle Royale series, is a belt of
amygdaloids similar in general particulars to those of the Pewabic
group. Itincludes two great lodes:—the grand Portage, worked in the
mine of the same name on the south shore of Portage Lake ; and the
isle Royale, which is opened on the Huron mine, also on the south
side, but has also been traced for several miles on the north shore.
Ht is a pale-green amygdaloid containing quartz, steatite, chlorite,
epidote, and copper in small quantity, from 24 to 33 feet in thick-
néss, ylelding about I per cent. of copper when dressed. Below the
Isle Royale is another lode called Mabbs lode, which has recently
been discovered ; and it is not quite certain whether it be a parallel
belt or an actual fissure-vein, as its dip is much steeper, being 75°
instead of from 52° to 60°, which is the amount of inclination of the
higher belts.

6. Mines of the Northern District.
Point the cupriferous amygdaloids occupy but a Eibordinste Coste
the whole of the produce being derived, with a very few exceptions,
from true lodes, or, as they are called in the district, fissure-veins,
which, as a rule, are nearly vertical, and cross the trappean formation

VOL, XXII,—PART I. pag

456 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Aprair,

atright angles to its strike, the greater number being included between
the directions N.W. &S.E., and N. &8. The relation of the rocks is
shown in the sketch-section, Fig. 4, from which it will be seen that.
the trappean series is divided into two parts by the great greenstone
bed, the upper portion being known as the northern, and the lower
as the southern mineral range. Now although lodes in many cases
pass through both ranges, yet, as a rule, up to the present time they
have rarely proved to be of value for copper in both, the most im-
portant deposits being confined to the southern side, and at no great
distance from the greenstone, the principal mines being the Cliff near
Eagle River, the Amygdaloid, Delaware, and Pennsylvania near
Eagle Harbour*.

Fig. 4.—Section from Copper Harbour to Lac la Belle
(after Foster & Whitney).

i=)
$ 2
ea oo 8
oa 3 ; =
Copper 20 5 Bohemian Q
Harbour. oF} Mountain. pal

SY...--. Montreal
River
eoaase eS UpeTOrs

oe Belte:
f._.____- Sandspit.

a. Upper sandstones and traps, | ce. Lower metalliferous traps.

6. Upper metalliferous traps. d. Chlorite rock and sandstone.
e. Porphyry ?

The lode worked at the Cliff mine has been traced for about 23
miles, but the main workings are below the greenstone, and extend
southward for about 1400 yards. It is a nearly vertical fissure,
varying in breadth from a mere line to six feet, filled with broken
rock and zeolitic minerals, with native copper, both in fine particles
and large masses, the latter being common in the wider portions,
which alternate with barren strings made up of laumonite and de-
composed trap. The containing rock is a hard trap, with interstra-
tified beds or “flows ”’ of amygdaloid, which have been laid down
in the plans to the number of 12 or 13. These are occasionally

* The total yield of copper from the mines of Lake Superior in 1864 was
as follows :—

From 13 mines in Portage Lake district, 4293 tons of 70 per cent. mineral.
se le », Keweenau re 2548

ae 4) a Ontonagon 1722 a

8563 tons.

These quantities are in American customary tons of 2000 lbs. The above
total is equal to about 5609 statute tons of fine copper.
The largest individual production was, in dressed mineral (70 per cent) :—

1485 tons 13 ewts., American weight, from Quincy Mine.

TSS n ua Loe. os a Cliff Mine.
Go2uee Si heh, - Me Pewabic Mine.
609 _,, or af , ¥ Central Mine.

D2D eee ae ¥ ‘ National: Mine,

1866. ] BAUERMAN—COPPER-MINES OF MICHIGAN. 457.

impregnated with copper to a depth of about 20 feet from the lodes.
The mine is 156 fathoms deep, and produces from 35 to 65 masses
weighing about a ton each per month, and about an equal weight
from stamp-rock, containing about 1:9 per cent. The copper-ground,
as a rule, appears to follow the greenstone in depth, dipping about
27° north-westerly. The North and South Cliff mines, opened on
the prolongations of the same lode, are not now at work.

The Central mine, about 14 miles east of the Cliff, is opened upon
a similar lode, consisting of a series of alternations of red laumonite
strings, with large lenticular expansions contaming copper. The
original discovery of this lode was made in an old Indian working at
the No. 2 shaft, out of which a mass of copper, weighing 50 tons,
was taken. Only a small amount of metal has been found imme-
diately below this point in sinking; but further north, below the
greenstone, under similar conditions to those observed in the Cliff
mine, a very rich run of ground has been discovered. There is a
good deal of calespar in the vein, and the finer copper appears rather
in sheets than in shots. At the 50-fathom level, on the No. 4 shaft,
the largest mass that has as yet been discovered on the lake was
struck ; it measured 50 feet in length, 30 in height, and about 44
feet in greatest thickness, and yielded somewhat over 500 tons of
copper.

Fig. 5.—Longitudinal Section of the Central Mine.

No. 1 Shaft. No. 2 Shaft. N.15°W. No. 4 Shaft.
i i =>—> :

“

SAD aS
ay “ Ny oe SOT aS SO.
: Ve NTR,

Wi.

7 L cet Uy Vili
2 MM. hn. \__>

60 aw oe

The mines in the range north of the greenstone are the Petherick,
Copper Falls, and Phoenix, which derive their produce almost entirely
from a remarkable bed of very much decomposed finely vesicular
trap, filled with small shots of copper, known locally as the “ ash-
bed.” Associated with this is a compact trap, containing elongated
cavities at its contact with the more vesicular portions. These
cavities are usually filled with copper in ramifying forms resembling
eagles’ claws. The ash-bed, according to its discoverer, Mr. Hill,
has been traced for about 8 miles, and by its position probably
represents some of the upper beds of Portage Lake. Although ex-
tensively worked, it is too poor to yield any great profit, the produce
at Copper Falls being 1 per cent., and at the Phoenix only 2 per
cent., of the rock treated.

212

458 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Ape a1,

7. Ontonagon District.—The mimes of this district are all opened in
the same class of deposits—-namely, very irregularly defined lodes
which follow the strike of the trappean belt, commencing on the
Minnesota Hills, at the southern end of the district, which rise
abruptly from a drift-covered plateau, about 12 miles in length,
lyimg to the south of the town of Ontonagon. They extend in a
north-easterly direction for about 16 miles to the Wynona mine, the
last explorations im the direction of Portage Lake. The Minnesota
mine has been worked to a depth of about 200 fathoms, on a lode
dipping about 46° northerly, and included between a roof of compact
grey trap and a floor of conglomerate. A northern branch, dipping
at a higher angle, falls into it at the fifth level below the adit; be-
tween these is another branch, more nearly parallel with the main
lode, m which the great mass of 400 tons was found im the year
1856, about 20 fathoms below the surface. This mine has shown
a, decided decrease of richness in depth, the produce having diminished
from 2058 tons in 1857, derived from ground yielding 1267 lbs. per
fathom, to 3874 tons in 1864, the amount. per fathom being reduced
im the latter year to 186 lbs. The lower workings are now com—-
pletely abandoned, and an attempt is being made to develope the
northern lodes. As seen in the adjoining National mine, the Minnesota
lode is filled with a mass of epidote and quartz, apparently of a
brecciiform structure, with rough particles of copper scattered irre-
gularly through it. The hanging wall is full of small slipped pieces.
of rock and clay, and is covered with longitudinal striations.

The sandstone below the conglomerate on the underside of the
lode occasionally contains a little copper, when it assumes a lami-
nated appearanee, in thin stripes of red jasper and yellow epidote
grains, interspersed with bright metallic leaflets, the arrangement
being similar to the cement of the Albany and Boston conglomerate
and the compact epidote-rock of the Porcupine Mountains.

The lode at the Indian mine is anepidotic mass, apparently a con-
eretion in the hornblendictrap. It is remarkable for carrying large
quantities of analcime, with small masses of copper in solid crystals.
A very decided concretionary structure is seen in the trap at the
Bohemian and Toltee mines, which are on the same run of ground ;
the deposit worked is a course of trap, filled with epidote about 8 feet
thick, the rock containing spheroidal masses which in section pre-
sent alternately light- and dark-green rings, the former being due
to epidote, and the latter to the prevalence of hornblende and chlorite,
the two colours being divided by intermediate rings of calespar: the
largest of these concretions are about 15 mches in diameter. The
lode is an epidotic amygdaloid, about 8 feet in thickness, with a
N.W. dip of 35°. It is spotted through with small strings of
ealespar and quartz ; the copper occurs either in pseudomorphs or in
crystallized masses of no great size, or in leaf-like plates in the bright-
green epidote: similar conditions prevail in the Wisconsin mines fur-
ther to the N.E.; but as yet none of these mines are distinguished by
any great production. Several heavy masses have recently been taken
out of the shallow workings at the Flint-Steel mine, which is opened

1866. ] BAUERMAN—COPPER-MINES OF MICHIGAN. 459

upon an epidote-breccia lode divided into two branches by a horse
or rib of barren trap. Very extensive traces of aboriginal mining
have been discovered at this place, the old miners haying sunk their
pits on both branches of the lode, avoiding the barren ground between
them. Itis very remarkable that almost all the valuable mining
locations on the lake show traces of Indian or Aztec work; and
recent discovery has shown that they not only worked on the mass
lodes, but. also—in one instance at least—on the conglomerates. If
the country were less wooded, these old workings might be of consi-
derable service in indicating the position of deposits of value; but
they are, in almost all instances, filled up and covered by vegetation,
the trees being as large as any of those of the surrounding forest,
thus giving proof of the remote antiquity of these workings.

8. Paragenesis.—The following are a few of the chief alternations of
minerals observed in the Lake Superior mines: others will be found
in the works of Professor Whitney :—

Chlorite, calcite, copper—Pewabic lode.

Chiorite, quartz, copper—Isle Royale lode.

Chalcedony, quartz, apophyllite, calcite—Bay State mine.

Laumonite, quartz, green-earth—Phcenix mine.

. Prehnite, quartz, copper, laumonite—Bay State mine.

. Natrolite, lanmonite, analcime—Copper Falls mine.

. Calcite, copper, analcime, orthoclase—Copper Falls mine.

. Apophyllite, copper, orthoclase—Copper Falls mime.

. Datholite, copper, calcite—Copper Falls mine.

10. Analeime, copper, orthoclase—Bohemian mine.

11. Quartz, prehnite, copper, calcite, clay—Albany and Boston lode.

12. Quartz, epidote, laumonite—Isle Royale lode.

13. Quartz, epidote, copper, orthoclase, calcite, melaconite—National mine.

14. Calcite, prehnite, copper, cuprite, chalcotrichite, chryosocolla, allophane,
silver—Albany and Boston conglomerate.

15. Calcite, chrysocolla, malachite, cuprite, silver—Albany and Boston conglo-
~merate.

16. Quartz, Whitneyite—Shelden and Lexington mines.

17. Copper-glance, caleite—Mendola mine.

DOM duh ON =

From the above list it will be seen that the copper is sometimes
older and sometimes newer than the associated minerals. In the
Ontonagon district it occurs very generally as incrusting pseudo-
morphs upon opaque rhombohedra of calcite, but is also itself
enclosed in transparent complex scalenohedral forms of the same
mineral, but of later formation. Similar encrusting pseudomorphs of
quartz are also common, the original mineral having at times been
removed, leaving an empty six-sided tube. The best examples of
this class are to be found at the Huron and Bohemian mines.
Silver occurs, both in massive lumps included in the copper and in
crystallized arborescent forms. The two metals have probably been
deposited simultaneously.

9. Origin of the Copper.—The occurrence of native copper in the
cavities of amygdaloid traps has been observed under circumstances si-
milar to those seen on Lake Superior, in the agate-bearing melaphyre
of Oberstein in Rhenish Prussia, in Nova Scotia, and in the Faroe
Islands. Thin sheets encrusting the walls of cracks in similar rocks

460 PROCEEDINGS OF THE GEOLOGICAL soctery. [Apr. 11,

have been found in several places near Glasgow. In the whole of
the above localities, however, it is a comparatively rare phenomenon,
and might be accounted for by the reduction of dichloride of copper
sublimed from a volcanic vent—a process of which we have indica-
tions in the occurrence of oxychloride of copper in the lavas of
Vesuvius. It is difficult, however, to consider this an adequate
cause for the metallization of a mass of rocks which, from their
appearance on Isle Royale, Michipecoton, and other points on the
northern and eastern shores of the lake, must cover an area of many
thousands of square miles. Another hypothesis, suggested by Miller,
supposes the copper to have formed part of the felspathic component
of the trap rock when in the unaltered state—a view that is sup-
ported by the occasional occurrence of protoxide of copper in small
quantities, usually less than | per cent., in several anhydrous silicates,
such as felspar, orthoclase from Schemnitz, and Amazon-stone from
Siberia, epidote from 8. Marcel in Piedmont, idocrase in the Nor-
wegian variety called cyprine, and olivine*. 'This hypothesis may
be modified by supposing the copper to have existed in the trap as
sulphide, mechanically interspersed in minute quantities, in the same
way that it is found in the coarse metal slags of copper-furnaces. On
the other hand, we have the recorded statement of Whitney, who,
in an analysis of the trap from Isle Royale, found it to contain no
copper, although it was specially sought for; but traces were found
in the sandstones overlying the trappean series. This piece of nega-
tive evidence, however, must not be overestimated, as it would in
any case be very difficult, if not impossible, to determine the original
composition of the traps as they exist at present. They have un-
doubtedly undergone considerable change, as is shown by the presence
of hydrated minerals, such as chlorite and zeolites, as well as calespar.

Rammelsberg has found as much as 0:56 per cent. of protoxide of
copper in a lava from Vesuvius from the eruption of 1811—a rock
not very dissimilar in composition from the Lake Superior trap; and
although we have great masses of copper concentrated at single
points, it must be remembered that the percentage contents of the
deposits selected as rich enough for working are included between the
narrow limits of one-half and two per cent.; and supposing the con-
tents of these deposits to be uniformly distributed through the whole
mass of the traps, the state of division would be so great as to render
the copper difficult of detection. The presence of copper in the sand-
stones suggests another origin—namely, that it may have originally
been deposited with the quartz-ore sediment as a finely divided sul-
phide from sea-water under the influence of organic matter, and by
subsequent oxidation and solution have been removed and collected in
the rocks below. Cupriferous sandstones and other sedimentary rocks
are comparatively common, as, for example, the Carboniferous Sand-
stones of Nova Scotia and:the Kupfer Schiefer, which contain sul-
phides of copper in an unaltered form, partly on account of the state
of aggregation of the deposited mineral, and partly from the texture

* Bischof, Geol. vol. ii. pt. 3. p, 189.
t- Geology of Lake Superior, pt. 2. p. 87.

1866. | BAUERMAN—COPPER-MINES OF MICHIGAN. 461

of the rock and the presence of organic matter, which prevents oxi-
dation. In coarser and more easily permeable rocks, however, not
containing organic matter, it is easy to see how the finely divided
sulphide would be readily oxidized by infiltrated atmospheric water,
giving rise to sulphates, carbonates, and other oxidized minerals—a
condition which is exemplified by the cupriferous Triassic Sandstones
of Cheshire, which contain only oxidized compounds of copper.

The size of the accumulated masses of metal appears to be mainly
dependent upon the size of the cavities in which they are deposited,
whether in the amygdaloids or in the main fissures ; and their absence
in the compact traps 1s probably only due to the non-occurrence of
such cavities. In almost all cases the introduction of the metal has
been preceded by the deposit of minerals produced from the decom-
position of the rock, such as quartz, calcite, chlorite, and zeolite; and
in the larger cavities it is often followed by transparent crystals of
calcite, which are formed over branching masses of copper, or even
show signs of simultaneous deposition, being filled with fire-spangles
of metal arranged parallel to the diagonal striations or lines of growth
on the rhombohedra. Similar alternations in the formation of
zeolites, more particularly analcime, have been described by Whitney.

Bischoff* has shown that hydrated silicates of copper, both
artificially prepared and the natural mineral dioptase, are sensibly
soluble in pure water, but much more readily so when carbonic acid
is present, the solution in the latter case being attended with a par-
tial decomposition and separation of silica. <A reaction of this kind
is suggested by the occurrence of chalcedonic and quartzose kernels
in the amygdaloids of the higher portion of the trappean series, while
copper is found lower down. As regards the reduction of the metal
from solution, it is probable that the chief agents have been sub-
stances containing protoxide of iron derived from the decomposition
of the trap itself. Professor Andrews, of Belfast+, has suggested a
more potent reducing-medium in the presence of metallic iron in
certain varieties of basalt in Ireland, and other crystalline rocks
from other localities; but it does not appear to be very likely that
‘such an agency can have been at work on Lake Superior, as it is
difficult to suppose that an eminently oxidizable substance like finely
divided iron could have remained unaltered after the changes pro-
duced by infiltration of water had once been set up; and these
changes appear to have preceded the deposition of the copper.

A point of considerable interest, but which we have at present no
means of determining precisely, is, whether the copper in the fissure-
veins is of the same age, newer, or older than that of the amygda-
loids of Portage Lake. I am inclined to think that the latter are
the older class of deposits, and that they have served as feeders for
the fissure-veins, for the following reasons :—

1. The lodes carry more copper between amygdaloid walls than
they do when encased in compact trap.

2. The transverse joints and fissures of the amygdaloids on

Voli. pt. dopey Sez. + Brit. Assoc. Report.

462 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Apr. 11,

Portage Lake carry masses and sheets of copper analogous bis but .
much smaller than, the masses of the northern mines.

3. The amygdaloids adjoining the bearing portions of the veins are
often found to contain considerable quantities of copper for some
distance from either wall.

The last of the above reasons may no doubt be made available in
support of the opposite hypothesis of the permeation of the cellular
rock by materials introduced from the lodes; but in order to prove
this, it would be necessary to show that the rock was barren, except
within the distances explored. This is, however, by no means cer-
tain, as the miner stops at the limit of profitable working without
carrying on systematic researches along the strike of the bed, as is
done in the Portage district.

Bischoff * showed, as far back as the year 1825, that copper may
be deposited from solution in a massive condition in a compara-
tively short time, by the action of organic matter upon solutions
containing sulphate of copper partly in the state of a salt of the sub-
oxide. This was observed at Linz, on the Rhine, where a solid mal-
leable mass of copper, weighing 23 lbs., was deposited in a wooden
vat, used in the concentration of blue vitriol leys obtained from the
lixiviation of poor copper ores after roasting.

Where the amygdaloids are compact, and tolerably free from
eracks and joints, the metallic kernels have undergone no change,
and appear as clean brilliant masses on a freshly fractured surface.
it is different, however, at the outcrops, where the cavities are
usually empty, and their former contents, converted into malachite,
have been absorbed by the erystalline base of the rock, which is
stained green for a considerable distance round. Similarly in the
conglomerates atmospheric agencies have been largely at work, pro-
ducing malachite, red copper ores, chrysocolla, and similar secondary
products; and another instance of the same kind may be adduced in
the old vein in the sandstones of Copper Harbour, which yielded
melaconite and chrysocolla in considerable quantities, but not
metallic copper. The mines, as a rule, are very dry, the deepest
requiring only a small amount of pumping-machinery of no great
power, and that only employed at intervals, in order to keep the
workings free from water. This comparative impermeability of the
rock is probably the cause that has preserved its metallic contents
with such a small amount of change, as itis well known that metallic
copper is rapidly oxidized when exposed to ordinary atmospheric
vicissitudes. This is well seen in the “ floats,” or small masses,
that have been removed from the rock by denudation, and are found
in the drift covering the backs of the lodes. These are often in-
crusted with a coating of earthy malachite nearly half an inch in
thickness.

Perhaps the most interesting fact in connexion with the mineralogy
of the Lake Superior mines is the prominent occurrence of orthoclase
among the newest minerals in the lodes, and in succession to zeolites ;

* Pogg. Ann. in. p. 195.

1866. ] TYLOR-—VALLEY-GRAVELS. 463

and as it is found deposited upon the faces of erystals of analcime
and apophyllite, it is evident that it must have been formed at a
very moderate temperature *.

7 Aprit 25, 1866.
The following communications were read :—

1. Apprrtonat Documents relating to the Votcanic Ervrrions at
the Katment Istanps. By Commander Bring, of H.M.S. ‘ Racer.’

{Communicated by the Lords Commissioners of the Admiralty.]

(An abstract of this communication was published in Quart. Journ. Geol. Soc.
No. 87, p. 319, by order of the Council.)

2. Report fo the Eparcu of Santrortno on the Eruptions at the
Karment Istanps. By M. Fovaeus.

[Communicated by Sir R. I. Murchison, Bart., K.C.B., F.RB.S., F.G.S8., &e.

’ {An abstract of this communication was published in Quart. Journ. Geol. Soc.
No. 87, p. 320, by order of the Council.)

ae

3. Remarks upon the Inrervat of Time which has passed between
the Formation of the Upper and LowEr VALLEY-GRAVELS of part of
Enexanp and France; with Notes on the Character of the Hons
bered in Rocks by Motxiusca. By A. Tytor, Esq., F.G.S.

Tue elaborate examination of the Quaternary deposits made by Mr.
Prestwich has induced that geologist to divide the valley-gravels
into upper and lower, which are supposed to be separated from each
other by a considerable interval of time.

There is much similarity in these deposits, although separated for
purposes of classification by Mr. Prestwich ; for the organic remains
are nearly identical, and the human implements found in both (made
of roughly chipped flint) are of the same general character. Mr.
Prestwich argues that although the upper valley-gravels are at a

* The following are the chief works on Lake Superior Mine :—

Foster and Whitney, ‘Report on the Lake Superior Land District,
Washington,’ 1845,

J. D. Whitney ‘The metallic weight of the United States.’

Rivot, “Voyage au Lac Supérieur,” Ann. des Mines, 5° sér. vol. vii.
p. 175; “Notice sur le Lac Supérieur,” Ann. des Mines, 5 sér. vol. x.

J ules Borie, ‘ Bulletin de la Société de l’Industrie Minérale,’ vols. vi.
Vil., Vill.

Alb. Miller, ‘ Verhandlungen der naturf. Gesellschaft zu Basel,’ vol. iii.

464 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 29,

higher relative level than the lower, yet the higher series are always
the older, and the lower the more modern; and we have thus the
ordinary superposition of new over old strata supposed to be reversed.
This difficulty is considered by most geologists to have been sur-
mounted by Mr. Prestwich’s arguments, and his classification of the
gravels has been generally accepted. My own opinion is, that .the
evidence on which Mr. Prestwich’s theory is based is insufficient ; at
the same time, I fully admit the careful and accurate manner in
which he has stated his views.

Present inquirers have the great advantage of having before them
the accurate sections prepared by Mr. Prestwich with great skill and
labour. Mr. Prestwich describes the drift-beds of the valley of the
Somme as the opposite extremities of a series of gravels deposited in
a period of time so vast that during its continuance extensive val-
leys were formed and excavated out of solid strata, and the gravel-
beds afterwards deposited on their flanks and on their bottoms.

The lower valley-gravels are more continuous than the upper ; and
their lower extremities touch the alluvium of the present rivers,
often on the same horizon. _

They contain organic remains resembling those found in the well-
known bone-caverns, including the bones of extinct Mammalia,
associated with flint weapons of rude workmanship. The upper
beds contain nearly the same organic remains and human imple-
ments as the lower, and are occasionally capped by thick beds of »
loess of freshwater origin. Both upper and lower valley-gravels
contain materials brought from a distance and deposited irregularly,
as if they were the feeble successors of the great diluvial deposits of
the glacial period which immediately preceded them, but which in its
typical form left no remains south of the Thames.

Mr. Prestwich has described the present valley of the Somme as
having a transverse section of five hundred times the area of the
present water-channel, and other valleys of similar character as
possessing still greater proportionate size when compared with their
present water-channels.

He supposes that during the elevation of the land the action of
torrents, ice, and snow removed large masses of stratified rock from
the valleys; and in writing of the duration of the period of time in
which the upper and lower gravels might have been accumulated,
he observes :—‘ The next possible standard to measure the dura-
tion of the period of time in which the upper and lower gravels were
accumulated is the time required for the excavation of the valleys
themselves.” I do not see that this supposition is confirmed by suf-
ficient evidence ; for, supposing the excavation of the valleys to have
occurred between the dates of the upper and lower valley-gravels,
we are obliged to allow not only a vast, but an apparently unneces-
sary amount of time for the accumulation of such incoherent and
often unstratified deposits. The lower valley-gravels at Grays,
Ilford, Menchecourt, &c. &c., are thick, and must be the accumula-
tion of a long period; for they contain remains in great abundance
of the large extinct Mammalia, deposited among fragile shells of

1866. | TYLOR—VALLEY-GRAVELS. 465

many Mollusca now living in tranquil water in the neighbourhood
and on the same horizon, and also of three species of Mollusca which
have disappeared from the country, one species not being met with
now at any nearer point than the Nile. To suppose that man was
living throughout the period of the lower valley-gravels at the same
time as the great extinct Mammalia, obliges us to carry back his
presence on the earth not only to a very distant date, but to a period
when physical circumstances must have differed very much from those
we experience. We therefore wonder that there are so few indica-
tions of his presence or works left behind; for we cannot realize the
lapse of time without fixing on some events by which to measure it.
If man existed prior to so great and distant an event as that of the
excavation of the valleys, the problem becomes still more difficult to
understand.

The opinion of Mr. Prestwich as to the age of the Somme valley
is not at present confirmed, as far as I am aware, by any other geolo-
gist. Sir H. T. Dela Beche thought the valleys of Devon and Corn-
wall opening into the English Channel might have been excavated
not later than in early post-Cretaceous times, but that their forms may
have been modified more recently. Mr. Godwin-Austen thinks the
German Ocean and English Channel were not united at the period
of the Coralline and Red Crag, so that the easterly part of the
Channel would have been formed in the Pleistocene period—a view
now generally adopted.

Also Mr. Pengelly considers that the valleys of the south-east of
Devonshire were excavated in post-Cretaceous times, and were sub-
sequently filled from base to hill-top—a point also discussed by Sir
H. T. De la Beche without his arriving at a definite conclusion*.

Mr. Pengelly distinctly refers the reopening of the valleys to a
subsequent denudation, and remarks, ‘‘ A remnant of the gravel re-
mains to line the slope and preserve a record of the operations” f.
He does not give any sections; but, having visited some of the local-
ities, I concur entirely in his opinions. Mr. Pengelly asserts that he
has also discovered perforations made by a marine boring-animal at
considerable elevations above the sea and above raised sea-beaches,
in many localities in the Torbay district; and I give the following
sections of valleys, that the position of these bored holes may be
clearly understood.

In the valley leading to Kent’s Hole Cavern (fig. 1) there is red drift
on the plateau, and the same material in the cavern and on the bottom
of the valley; this is usually the case in the district. If the borings
in the limestone forming the face of the cliff in which the openings
into Kent’s Hole Cavern occur, at a height of 180 feet above the sea,
have been made by a marine animal (Pholas, or any other borer)
then it is good evidence that the drift has been removed from the
narrow and short valley below the cave, leaving no marks of denu-
dation on the valley itself. We have therefore no evidence in Kent’s

* I may add that the fringes of gravel along the Devonshire valleys were

a tice by Mr. Godwin-Austen in an early paper.
+ ‘Denudation of Rocks in Devonshire,’ 1864, p. 19.

466 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 25,

Hole valley of such a great denudation as Mr. Prestwich supposes
to have occurred in the valley of the Somme, although we have in
both places drift associated with the bones of extinct Mammalia,
and with rude flint implements at very high levels above the sea.

Fig. 1.—Longitudinal Section of Marychurch Valley.
E.N.E. W.S.W.
Marychurch.
i g50ff
ea

me
-——
—«

* Pholas markings.

The raised beaches fringing the coast-line in the south-east of
England, north-east of France, and south-east of Devonshire, as
well as the gravels, &c., fronting at similar heights the transverse
valleys which open in both districts into the English Channel, place
all these localities in close geological relationship.

The presence of calcareous deposits on the sides of the chalk val-
leys in France, described by Mr. Prestwich, is matched in Devonshire
by a calcareous deposit which has cemented loose blocks of limestone
on the solid rock.

At Watcombe, figs. 2 &3, one mile north-east of Kent’s Hole Cavern,
the analogy is still more complete, if I am correct in the suggestion
that this may be a thick bed of freshwater loess covering the angu-
lar drift below it, and that both drift and loess are derived from the
ruins of the Triassic rocks close by. The clay in question is ex-
tremely fine, and must have been deposited from a most tranquil
lake +; and yet it 1s now raised more than 200 feet above the present
sea-level.

Fig. 2.—Longitudinal Seetion along the Valley of Watcombe.

W.S.W. E.S.E.
Sea. Road.

.
1

SP ee es

SS
Shy 2A: ye
Tumbled Rock.

Level of Valley.
Fig. 3.—Coast-section from Babbacombe to Watcombe.

‘S.S.W. ENE.
eee 4c0 ft ere
GFE Nines hx
oN genet eet: loess Hi;
ZL? 0 a, : AN YZ
EN a5, iy Ja i
x Borings.

Reasoning on so many parallel circumstances, we must admit a
close analogy between the former condition of the Devonshire and
Somme valleys during the gravel-period, and may consider that the
surface of the Devonian limestone has been so little affected by the

+ This loess clay is about to be used for terra-cotta figures.

1866. ] TYLOR—VWALELEY-GRAVELS. 467

action of weather during the removal of the gravel in the valley above
and below it that the interval must be comparatively small since the
event in question tvok place, viz., since the valley previously filled with
gravel, sand, or mud was denuded, leaving what may be called high-
and low-level gravel in a remanié state on the flanks and the bottom.

Having repeatedly visited the valley of the Somme without being
able to satisfy myself as to the correctness of the views entertained
by geologists regarding the extreme antiquity of the upper gravels,
I wish to state that I attach great importance to the views so long
ago put forward, as to the valleys of post-Cretaceous age having been
filled with gravel in one geological period and eleared out and par-
tially refilled m a subsequent and, perhaps, very recent date*.

The theory of the excavation of the French valleys between the
periods of the deposition of the upper and lower gravels was proposed
by Mr. Prestwich as the most probable explanation of the phenomena,
the impossibility of obtaining absolute proof of his hypothesis being
obvious.

All the evidence, on the contrary, which is forthcoming, [ peeaa
should rather cause us to admit the identification of the ages of the
Devonshire and Somme valleys ; for both sets of valleys are ancient,
they were afterwards wholly or partially filled with gravel, and the
gravel on the slopes and bottoms in each is remanié recently, the
levels of the new drift-deposits are similar, the character of the mam-
malian remains in each is strikingly alike, and raised sea-beaches
oecur on the coast not very distant from the mouths of the valleys
in question. If the perforations of marine boring-shells could be
proved to occur in the valley of the Somme, the analog gy would be
still clearer (but of this there is no evidence at the present time), as
it would then appear as if the deposition of these drift-beds might
have occurred almost within the historical period.

It is, however, certain that both the low- and high-level gravels
with human implements and mammalian remains are more re-_
cent than the Boulder-clay, for this is proved in’ the Hoxne section ;
and reasoning by analogy, all the other gravels in valleys and caves,
eontaining the same kind of organic remains associated with the
tools of uncivilized man, belong to an interval between the Boulder-
clay and historical periods.

The raised sea-beaches containing only organic remains of spe-
cies of mollusca now living in their neighbourhood are the equiva-
lents in time of a portion, or the whole, of this period—as their sub-
aerial heads shade into modern deposits, while the base may, from
other reasons, be of much older date. Godwin-Austen separated the
lower portion of the Brighton beach from the upper, many years since,
in this manner.

The conclusions at which I arrive are :—

1st. That the valleys of the south-east of Devonshire and of the
north-east. of France were excavated in remote geological periods,

* Pengelly, Denudation of Rocks in Devonshire, p. 13.
Tt Prestwich, Phil. Trans. p. 253, 1864.

468 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

and filled up with marine or fluviatile gravel, and reexcavated prior
to the epoch of the high- and low-level valley-gravels.

2nd. That all these gravels are reconstructed of drift and gravel
of the Glacial period, or of its equivalent south of the Thames, mixed
with a certain amount of local materials.

drd. That the high- and low-level gravels are of one formation,
closely connected in age, and dating from a time immediately pre-
ceding the historical period.

May 9, 1866.

The following communications were read :—

1. On a New Spxcres of Acantuopss from the CoaAL-SHALES of
Loneton. By Sir Puirre pe M. Grey Eeerron, Bart., M.P.,
iG. E.G-S., ce.

[Puate XXITT.]

Owine to the kindness of Mr. Ward, of Longton (who has for some
time past devoted his time and attention to collecting the fossil
remains of the coal-pits in his vicinity), I have had the opportunity
of examining a considerable collection of specimens of the Acantho-
dian fishes of the North Staffordshire Coal-measures. Numerically
speaking, the collection is a large one, but the specimens themselves
are all imperfect. The anterior parts of the fish are rarely pre-
served ; and even when present, the dislocations and crushed condition
of the component bones are so extensive that the form and structural
details of the head and thorax are difficult to decipher. Most of the
best-preserved specimens contain the middle and hinder portions of
the body, from the ventral spines to the bifurcation of the tail; and
all have the scales well shown, and most of the spines supporting
the fins. Although it might perhaps be desirable to wait for more
perfect specimens before undertaking a complete determination of
the specific forms, yet the evidence already procured is so decisive
as to the distinctness of at least one species, that a brief description
of this form may be given without prejudice to future investigation.

The generic characters of Acanthodes have been so thoroughly
worked out in previous publications * that it is needless to recapitu-
late them here, the more so since no important anatomical points
are supplemented by the specimens under consideration.

Selecting for description those individuals of a medium size, the
length of the body, from the snout to the point where the vertebral axis
trends upwards to form the upper lobe of the tail, seems to have been
about 54 inches. Of this total the anterior third comprises from
the nose to the point of insertion of the ventral spines, the middle
third from the ventral spine to the anal spines, and the posterior
third from the anal spine to the point above mentioned. Estimating

* Agass. Poiss. vol. ii. p. 9. Herr Fred. Romer, Ueber Acanthodes gracilis:
Breslau, 1857. Memoirs of Geological Survey, Decade 10. pp. 37 & 57.

1866. | EGERTON—ACANTHODES WARDI, 469

the length of the tail beyond that point at 14 inch, we arrive at a
total length of 7 inches for the perfect fish. The depth of the body
is greatest between the pectoral and ventral fins, where it measures
1}, imch. The anterior contour of the head is obtusely oval; and
the trunk tapers gradually from the thoracic region to the spring of
the tail. On comparing these dimensions with those of the known
species of the genus, it appears that this fish was far less bulky, and
more elongated, than Acanthodes Bronni from the coal of the neigh-
bourhood of Saarbriick, but not so slender as Acanthodes gracilis,
from the Permian beds of Klein Neudorf.

In one or other of the specimens the curious plates encircling
the orbit, the pair of slender ossicles representing the lower jaw,
and the branchial apparatus are well preserved. The orbital plates
are four in number on either side, and are prettily ornamented with
minute tubercles or granules. ‘They are very similar in character
to the analogous parts in Acanthodes gracilis. The styliform bones
ening the rami of the lower jaw are slender and rounded, and
about 2 of an inch in length. The branchial apparatus is com-
posed of six arches (as seen in one specimen), whereas Romer has
only represented four in his restoration of Acanthodes gracilis. They
are arranged more longitudinally, 2.e. more parallel to the outlines
of the back and belly, than in that species. ‘They seem to have been
unprotected by any opercular flap. ‘The pectoral spines are long,
broad, and scimitar-shaped, the distal end being flattened out and
rather blunt; a deep groove runs parallel to the anterior margin,
and a few obsolete depressions traverse the spine obliquely from the
inner pectoral margin towards the outer distal extremity: these are
not so prominent as the grooves on the pectoral spines of Acanthodes
gracilis. 'The spines are articulated to two strong T-shaped cora-
coids, a structural peculiarity common to all the Acanthodide, and
affording, according to Professor Huxley, one of the strongest argu-
ments against the placoid affinities of the family. The spines sup-
port fins of large size, the full extent of which is not shown in any
of the specimens. The ventral spines are situated, as before stated,
at one-third of the antero-posterior length of the fish. They are
short, sharp, and recurved. A distinct furrow runs along the front
of each. They bear small triangular fins. The anal spine is (next
to the pectoral spines) the most powerful of these defensive weapons.
It is long, thick, and nearly straight, and is traversed by a deep
groove. Itis furnished with a large fin extending to within one-
third of its point. The dorsal spine is inserted over and behind the
anal spine. It is rather weaker than that spine, and is slightly
recurved, but resembles it in all other respects. The tail is strikingly
heterocercal. The upper lobe tapers off to a fine point; the inferior
lobe commences below with strong fin-rays, which diminish in
length and strength as they ascend along the upper margin of the
lower lobe. They appear to be composed entirely of ganoin ; in fact ©
each segment has the character and appearance of a thick scale.
There is nothing remarkable in the dermal investment; the scales
are smooth externally, and have their under surfaces produced into

470 PROCEEDINGS OF THE GEOLOGICAL SO€IETY. [May 9,

small circular eminences. They increase in size as they recede from
the head, and are largest on the posterior part of the trunk. A
weil-defined lateral line traverses the flank about mid-distance
between the back and belly, and an auxiliary mucous duct runs
along the abdominal parietes as far as the anal spine.

I am desirous of giving my testimony to the zeal and liberality
which Mr. Ward has shown in advancing the knowledge of the
organic remains of his district, and therefore have much pleasure in
naming this rare species Acanthodes Ward.

Accompanying the specimens from the coal-shale are some iron-
stone nodules containmg remains of Acanthodian fishes, indicating
a species of much larger size than the one above described. |

One of these contains the head and anterior parts of a fish which
must have measured at least 2 feet 6 inches in Iength. Two other
nodules contain portions of the head of (probably) the same species,
a fourth specimen shows a pectoral spine 33 inches in length, which
may also have belonged to the same species.

The only other distinctive charaeter shown by these specimens is
the small size of the scales, they not being so large as those of Acan-
thodes Wardi, which species measured only 7 inches in length.

EXPLANATION OF Pirate XXIII.
: (Illustrative of Aeanthodes Wardt.}
Fig. 1.—Acanthodes Wardi. Natural size. In Mr. Ward’s collection.
Fig. 2.—Part of another specimen showing the branchial apparatus. Natural
size. In Mr. Ward’s collection.

2. A Sxercu of the Gravets and Drirt of the Frntanp. By Harry
Sertry, Esq, F.G.S., of the Woodwardian Museum in the Univer-
sity of Cambridge.

Part [.—Dzscriprive.
[ Abridged. |

By the Fenland is here understood the great flat country west of

the Chalk-hills of Norfolk, from Hunstanton to Cambridge, thence

to Bedford, and so north to Peterborough.

Such am area offers many conditions favourable for a consideration
of the subject of this paper, being bounded by Cretaceous rocks east
and south, and the outcrop of the Oolites flanking the west, while
the sea opens to much of the north; and the included country, being
nearly flat, presents a minimum of complications.

This tract slopes gradually to the sea, which it resembles in its
dreary uniformity. Every village and town, however, indicates a
patch of higher land than that around it; and from Chatteris, round
by Haddenham and Ely, to Littleport the level is relatively by no
means low. South of this, too, by Denny Abbey, Cottenham, Ramp-
ton, Over, and St. Ives, towards Huntingdon, there is a line of higher
ground. And south of this, to the east of Cambridge, are low Chalk-
hills, and to the west of Cambridge an undulating country of Cre-
taceous outliers and hills of Boulder-clay and Oxford Clay. All the
higher land north-east of Cambridge is capped with Shanklin Sand (?).

» JOUTN.LEOL.O0C.¥OL AAI Pi AAI

,
_

Vuar

M&N.Hanhart imp .

W.Dinkel lith

MWA IN THODE S

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Yeron :

WARDI .£

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1866. ] SEELEY—DRIFT OF THE FENLAND. 471

And the great level itself is the Fen-clay, in which are a few isolated
reefs of Coral-rag, and some stone-bands in its Oxford-Clay member,
which clay covers nearly the entire area.

There are in this region three kinds of drift—namely, a Boulder-
clay covering the high land, a coarse gravel which caps the hills,
and the fine gravel of the plains.

The Boulder-clay is widely spread to the west of Cambridge. It
rarely, if ever, forms hills, though frequently capping them. Yet
it is thick; for, near Caxton and Longstow, wells in it have been
sunk 160 to 180 feet: and the clay seems sometimes to fill up
valleys; for a well in the village of Caxton, half a mile north of the
deep sinkings, found the drift reduced to a thickness of 14 feet.

From March to Longstowe it is generally a dark-blue deposit
wholly unstratified, and more or less abundantly charged with frag-
ments of Chalk and Septaria and Limestone-rock of the ? Kim-
meridge Clay; while fragments may be found of almost any other
rock, though not everywhere. They abound at Longstowe; but a
little north, scarcely anything is found in it but chalk; while at
March the clay is almost free from fragments, and largely used for
brickmaking.

In this district, as elsewhere, it is rare to find gravel over the
Boulder-clay, though at a lower level gravel abounds. Thus the
high land of Elsworth, Papworth, and Abbotsley, is Boulder-clay ; and
the high land north of St. Ives, at Bluntisham &c., is Boulder-clay ;
yet all the valley between, as at Fenstanton, St. Ives, Hemingford
Abbot, &c., is filled with a fine flint-gravel. Where the Boulder-
clay ceases, at Elsworth, there the gravel begins, and thickens as it
joins the valley of the Ouse.

At Bluntisham the Boulder-drift presents the usual feature—
capping a hill. From it I obtained :—

Ammonites serpentinus. Gryphza cymbium.
bifrons. dilatata.

—— Marie. sp.

—— cordatus. Gime deltoidea.

—— biplex. leeviuscula.
Achilles. Cardinia Listeri.
Lamberti. Belemnites tornatilis.
serratus. abbreviatus.

— fimbriatus. , Liassic sp.
oxynotus. Belemnitella mucronata.

Pleurotomaria, sp. Terebratula subimpressa.

Gryphza incurva.

these species being characteristic of the Lias, Oxford Clay and Kim-
meridge Clay, and Upper Chalk.

The Boulder-clay at Ely is brown, and soueple for show-
ing, in places, regular courses of curved lines making a rough stra-
tification. But the chief importance of the section is in the fact
that, while the country above is level, the Boulder-clay has been let
down some 30 feet by a fault, thus evidencing considerable denuda-
tion since the Boulder-clay was deposited. It is also worth stating.

VOL. XXII.—PART I. 2K

472 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [May 9,

that many of the rocks of the north of England occur here*, and
among them great boulders of Mountain-limestone, such as are met
with at Elsworth and Wimpole. Boulder-clay also occurs on the
south side of the city, and on the landward side of most of the hills
in the Fens.

In the Museum of the Geological Society are a few shells from
March, Tellina solidula and Ostrea edulis, which were presented in
1846 by H. M. Lee, Esq. They are marked “ Raised beach.”

The deposit at March was subsequently examined by Professor
Liveing and the Rev. O. Fisher, who collected many fossils, and
presented them to the Woodwardian Museum. These also were
marked “ Raised beach.” But on visiting March in 1860, I found a
section 150 yards long, displaying a gravel included in the Boulder-
clay. The gravel was thin, a foot or so, though thicker east and

Hig. 1.—Section at March, in Easter 1860.

a. Boulder-clay, not very character- | e. Boulder-clay.

istic. b. Gravel. f. Gravel. jf’. Sand.
c. Many shells, but few species. g. Substriated Boulder-clay. Few
gq: Gravel. d’. Fine gravel. boulders.

west, and overlain, as shown in the section, by clay containing cha-
racteristic specimens of Septaria striated by drifting, hard chalk,
often deeply grooved as though by ice, and one bough of a tree some
3 inches in diameter, converted into imperfect lignite. The gravel,
which was largely made up of small pieces of flint and of sand,
contains an abundance of comminuted shells and many whole ones,
Tellina and Turritella being commonest. The Boulder-clay, where
seen underneath, has the usual characters. In the middle of the pit
the gravel, which was deeply ferruginous, end consisted largely of
small flint-fragments, came to the surface; and under this was a
layer much more sandy, with some rounded pebbles and few flints,
and half made up of shells. Buccinum, Trophon, Litorina, Cardium,
Tellina, and Ostrea were most abundant; and the greater part were
resting in natural positions. The deposit much resembled the Norwich
Crag of Thorpe, or of the Thorpe near Aldborough.

* The monks appear to have observed the peculiar character of the Boulder-
clay as early as the time of Henry the Sixth; forin Lonelich’s translation of the
Sank Ryal, a copy of which is in the hbrary of Corpus Christi College, Cam-
bridge, the description of a wound where the flesh had been burnt away to the
bone, is illustrated by the lines,

“And the bon as whit it lay,
Lik as doth chalk in the clay.”

1866. ] | SEELEY—DRIFT OF THE FENLAND. 473

_ Under the shell-bed was a very fine sand, which was cut-down-
into 4 feet. It is grey-brown at the top, but darker lower down,
becoming argillaceous, and at a greater depth changing to a blue-
black clay clearly stratified, which is dug for bricks. Out of this
clay were got Septarian concretions, and fragments of a large-grained
Oolite and other rocks. The pits are very extensive about the March
railway-station ; and everywhere the gravel contains shells, though
they differ from pit to pit.

Tracing this gravel south to Wimblingdon, near the railway-sta-
tion, the deposit, quite at the surface, and only a foot or two thick,
rests on one of those thin stonebands so common between the
Oxford and Kimmeridge Clays. It is a fine sandy gravel with the
usual shells; but the argillaceous-lhmestone rock was drilled with
the burrows of Pholades, the shells still being in the holes.

To the south the gravels are somewhat continuously spread along
by Chatteris, Somersham, Earith, St. Ives, Willingham, to Swaver-
sey. And in the spring of 1861, walking up the railway between
Over and Swaversey, I found the line had been made with gravel
dug on the spot, which was full of shells similar to those of March,
Tellina solidula and Turritella communis being very common, and
Cardium edule not rare. The pits, which were just beyond Drayton
Gate-house are, unfortunately, filled in. North of March the gravel
is continuous nearly to Wisbeach.

Marine Shells from March.

Rhynchonella psittacea.
Corbula nucleus.

Scealaria communis.
Trophon clathratus.

Astarte crebricostata. scalaris.

Mactra elliptica. Buccinum undatum.

Tellina proxima. Bela turricula.

Mya truncata. Turritella communis.
arenaria. Litorina litorea.

Tellina solidula. rudis.

Ostrea edulis. Natica helicoides.

Cardium edule. Natica, sp.

Purpura lapillus.

I will here notice a deposit at Hunstanton, as belonging to the
same geographical district. There are many pits between Hunstanton
and Brancaster where the gravel is thick and coarse ; but south of
the railway-station a hill has been cut into for ballast, exhibiting
ash-coloured sands and gravels 30 feet thick without reaching the
bottom. The cross stratification is very marked, and the beds differ
much in different parts of the pit. In some of the bands pebbles
were almost as well rounded as on a pebble-shore like Dunwich.
Shells occur in several distinct bands of gravel, and at various
heights, but are most numerous and best preserved in the coarse
layers.

This deposit is remarkable for the absence of local fragments
(the Red Rock occurs but rarely, and then only in small pieces
which may have come from the north); for the included fragments
comprise every kind of rock, numerous granites, syenites, traps,

2k 2

474 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

Cambrian, Carboniferous, Lias, Middle Oolites, Kimmeridge Clay,
Shanklin Sands, Speeton Clay, chalk and flint, and lignite, and
these in such proportion that it can hardly be called a flint-gravel.
Besides these are numerous balls, rough and round, formed of pieces
of clay which had rolled on a shore and so acquired a coating of
pebbles.

At the top is an earthy gravel with Ostrea edulis, Mytilus edulis,
Curdium edule, &c., very recent; for the Mytilus still preserved its
epidermis. |

The large shells were broken, and all showed marks of drifting,
in breakage, wear, or separation of the valves. Among others were :—

Buccinum undatum, ~ Mytilus edulis.

Nassa reticosa. Mya truncata.
reticulata. Scrobicularia piperata.

Fusus antiquus. Ostrea edulis.

Tellina obliqua. | Cyprina islandica.

Cardium edule. Corbula nucleus.

Associated with these were a Crioceras from the Speeton Clay,
Millericrinus probably from the Coral Rag, pieces of shelly Oolite,
Ammonites communis, A. annularis, and A. Bucklandii, a Lias
Belemnite, Gryphea imcurva, Carboncole, and Paleozoic Rhyn-
chonelle.

Southward to Lynn there is on the west a flat of Kimmeridge
Clay, and over this on the east is Carstone and sands, but so abrupt,
and so beautifully worked into chines, that one continually turns
round to look for the sea, now far away, which once wore and washed
them. Gravels occur all along, similar to those ferrugimous beds
spread about Lynn, and which extend south by Wallington.

Near Peterborough, at Overton Waterville (or, as it is called by
the country-people, Cherry Orton), is a pit which, although it has
been noticed, and plates of its fossils given, by Dr. Porter in his
“Geology of Peterborough,” I must here say a few words about.

There is much gravel round Orton; but, as Dr. Porter has re-
marked, it is only at this pit that shells are found.

In the section, which was some 12 feet deep, there is (1) earthy
gravel with the usual pipes, one of which is shaped like a flask.
These pipes descend into a gravel (2) with little sand, in which
the worn flint and Oolitic fragments rest flat, with vacant inter-
spaces—a feature also noticeable in several neighbouring pits. It
also, as do other local gravels, contains numerous dark shining
pebbles from the Carstone, but they are less numerous than at
Whittlesea. Below this is a shell-gravel (3) half made up of fluvio-
marine shells, from which my shells were taken. Then comes (4)
a brown clay, full of little calcareous concretions, but with few, if
any shells, though at its base I found one Rrssoa and one Cyclas;
but they may have belonged to the subordinate bed (5), which is a
marly slate-coloured clay, mottled with iron, with freshwater shells
scattered through it.

The drift-deposits already referred to are to the north of Cam-

1866. ] SEELEY—DRIFT OF THE FENLAND. 475

bridge. Those now to be noticed are in its more immediate —
bourhood.

East of Cambridge the fine flint-gravel reaches, by Granchester
and Comberton, nearly as far as the Boulder-clay of Stow, being
here deposited on the Gault.

North of Cambridge it extends in a continuous bed by Barnwell,
Chesterton, Histon, Oakington, Long Stanton, Landbeach, Water-
beach, Denny Abbey, and in a less continuous belt nearly all the
way to Ely. At Comberton, teeth of the Tichorhine Rhinoceros
have been found; but it is only from a few pits that bones can
be collected, though at Barnwell and Chesterton they are not rare.
I have found shells in the gravel under the Observatory on the St.
Neots Road, at Barnwell, Chesterton, and Oakington ; but in every
case they were land or freshwater forms, though from the gravel of
Waterbeach the Woodwardian Museum has a vertebra of a whale,
which, from its preservation, was evidently contemporaneous with
the formation of the bed. It has lost its epiphyses, and is seemingly
worn.

At and beyond Trumpington the gravel is remarkable for the great
extent to which its upper 2 or 3 feet are contorted and folded,
as though by lateral pressure. Except in some so-called brick-
earths near Hadleigh in Suffolk, I never saw more marked instances
of the kind on a small scale. But the gravel- flexures may only in-
dicate the site of an ancient forest.

About Cambridge the chief pits are at Barnwell and Chesterton,
where the gravel often shows a large amount of false bedding, which
varies greatly from year to year.

This gravel consists chiefly of small flint-fragments, generally with
sharp angles, often with the angles rubbed off; and rarely specimens
may be found which are well rounded. It is no uncommon thing
to find a flint well worn on one side, but with the others showing
fractured surfaces, which fact clearly indicates that the flint was
already a worn and drifted boulder before broken up to form gravel.
Phosphatic nodules and shells of the Greensand are not rare; and
many of the smaller fossils of the latter bed may be found in the
Barnwell gravel in vast numbers. Upper Chalk fossils are common.
lias gryphites, greatly worn, are numerous; and the Oxford-clay
gryphites in fragments are not rare. 1 have found some corals like
those of the Coral Rag. The rock-specimens which have come
from great distances are rarely large. The largest block which I
have seen from Barnwell, measured about a foot and a half in
each diameter, and was probably from the Shanklin Sands. Jas-
per conglomerate is found in angular blocks of a few inches dia-
meter. Granites of various kinds, syenites, and traps of various
characters, some of them amygdaloid, are among the common “ig-
neous” rocks, occurring in partly rounded boulders from 3 to
about 9 inches in diameter. There are fragments of Oolitic Lime-
stone. But all these are comparatively rare, and might pass un-
noticed, but that in sifting the gravel they are necessarily thrown
out. At Chesterton they are much more abundant than at Barn-

476 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

well, though the pits are but a mile apart and the gravel is con-
tinuous; but the level is a little lower.

Examined generally, the gravel is formed of layers which extend
pretty continuously round the pit. The lowest layer exhibited is
quite a coarse bed, with pebbles, mostly rounded. About two feet
above this is a bed of yellowish-brown marl, almost clay, irregular in
thickness, from a few inches to four feet. At times cuttings display
one or two similar but thinner beds in the upper part of the section.
The lines of bedding are partly marked by change of material, but
for the most part by infiltration of the red oxide of iron.

The most important stratum is the marl-bed, first described by the
Rev. P. B. Brodie; for in this are found fragments of plants, seed-
vessels of Chara, and many shells, some freshwater, others land forms,
nearly all now living in Britain, and only a few differing as varieties
from the common English species. Here, too, are found the bones of
various mammals, probably all, or nearly all, extinct ; and in the same
bed is evidence of man in his work. The gravel-diggers state that
the bones are generally found in the marl-bed. Neither the friable
shells, nor the larger bones, seem much, if at all, worn.

It had long been a matter of astonishment that the bed had never
given any evidence of a carnivorous animal; but my friend, Mr.
Dewick, of St. John’s College, first supplied the evidence of their
existence by finding a phalange; and Mr. Farren afterwards
showed me a- well-preserved jaw of the great Cave-tiger from
Barnwell.

The bones from Barnwell are :—

Bos.—Right os calcis, distal end of left femur, right and left me-
tatarsus, left astragalus, and glenoid end of scapula.

Equus.—Distal end of right tibia, hoof, 1st phalange, and 2nd
phalange, distal end of left humerus, and teeth.

Cervus (megaceros, var.).—Distal end of left tibia, distal end of
metacarpus, right astragalus, distal end of left humerus, cranium,
palate, and left tibia, antler, &e.

Cervus (small).—Scapula and left os innominatum.

Rhinoceros (tichorhinus).—Last premolar right side lower jaw,
penultimate molar right side upper and lower jaws, penultimate
molar left side upper jaw, and last molar right side upper jaw ;
right astragalus, 6th and 7th cervical and anterior dorsal vertebre,
right tibia (very young), proximal end of left radius, right condyle
of left femur, middle left metatarsal, distal end of left humerus, left
tibia, and cranium.

Elephas prinugenius.—Fourth metatarsal right leg, middle meta-
carpal right leg,;femur, carpal, last true molar right side, set of
molars, tusks large and small, and cervical vertebre.

Elephas antiquus.—Molar lower jaw.

Hippopotamus.—Right os calcis, left os calcis, and incisor tooth.

The land and freshwater shells of Barnwell are given from a list
prepared by Mr. Dewick from the specimens in his own collection,
which is the best yet made :—

1866. ]

SEELEY—DRIFT OF THE FENLAND.

Last of Land and Freshwater Shells from Barnwell.

Spherium corneum, Lin.

Pisidium amnicum, Mill.

—— fontinale, Drap. The typical
form occurs together with var. Hen-
slowana.

Unio pictorum, Lin.

rhomboideus, Schrot. Many spe-
cimens still retain the ligament.
One occurred of almost circular
form (L. 1:5 inch; B. 1:9 inch).

Cyrena fluminalis.

Hydrobia marginata, Mich.

Bithynia tentaculata, Lin.

Valvata piscinalis, Mild.

cristata, Miill.

Planorbis nitidus, Mill.

glaber, Jeff.

spirorbis, Miill.

vortex, Lin.

complanatus, Lin.

contortus, Zin.

Limnea peregra, Mill.

auricularia, Zin.

palustris, Mi//.

truncatula, Mill.

Ancylus fluviatilis, Mid/.

Succinea putris, Lin. Some of the
forms approach 8. elegans, Risso.

Zonites cellarius, Mild.

Zonites nitidulus, Drap.

nitidus, Miill.

fulvus, Mill.

Helix nemoralis, Lin:

arbustorum, Zin. Both the typical

form and the var. alpestris, as well as

intermediate varieties may be easily

found.

hispida, Lin. Very common. ‘I

found one specimen with reversed

spire.

ericetorum, Mill.

—— rotundata, Mill.

pygmea, Drap. Common.
occurred with reversed spire.

Bulimus montanus, Drap.

Pupa marginata, Drap.

Vertigo antivertigo, Drap.

pygmeza, Drap.

Moulinsiana, Dupuy. (Mr. J. G.
Jeffreys nas kindly verified this de-
termination, and says that it “ cor-
responds in size with continental spe-
cimens.”)

Clausilia rugosa, Drap.

—— biplicata, Montz.

Cochlicopa tridens, Pulteney.

lubrica, Mild.

Carychium minimum, Mill.

One

We here find, as in other contemporary deposits, Cyrena flumi-

nalis, Hydrobia marginata, and Unio rhomboideus, which have now
become extinct in England. Vertigo Moulinsiana has been once
met with by Mr. Jeffreys in Ireland, but has not hitherto occurred
in England.

The shells are mostly in a very good state of preservation. The
Helices retain their bands of colours, and the bivalves are generally
found with united valves.

March 15, 1866. Epw. 8. Dewicx.

The evidence of the existence of man consists of a cut bone. The
specimen is a second rib, like that of an elephant, and was ob-
tained by the Rey. F. J. Blake, M.A., of Caius College, in the spring
of 1862. The greater part of the bone is wanting, having been
severed at about three inches from the articular end, which part
only is preserved. This fossil shows on the severed end numerous
cut surfaces, evidently made with some sharp instrument used by a
powerful hand. The facets extend all round the end; and it is not
impossible that they were made to facilitate the breaking of the bone,
much as one would notch a broomstick before putting it across the
knee. The specimen is beautifully preserved, and does not show a
trace of attrition or gnawing, nor are there on it any othercuts. It
is in the usual condition of Barnwell gravel-fossils, of a pale rusty-
yellow colour, slightly glossy, and has lost most of its animal matter.

478 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

There is no doubt that the whittling is as old as the bone; for, be-
sides the fact of the cut surfaces having the same features as those
which are natural, and their very existence being unknown until the
fossil came into my hands, there is the satisfactory circumstance of
a few of them being covered with a stalagmitic deposit ; moreover
these facets are slightly concave, as if shrunk from the animal matter
having been subsequently removed.

It occurred twelve feet deep, in the freshwater stratum of Barn-
well, associated with remains of Elephant, Rhinoceros, and Hippo-
potamus.

There is another class of facts in connexion with this gravel
worth remark; and that is, the “ pipes” and what I shall name
‘‘walls.” The pipes vary much in size and length; the particles
of gravel generally dip towards them, though in one instance the
edges of these beds on each side were directed wpward—which I can
account for by a gaping of the gravel, and material falling into the
hole while it was closing, or by the forcible uprooting of a tree.
The walls extend from the top to the bottom of the pits; they are
more uniform in width than the pipes, and are usually hard, so that
when the gravel is dug away they stand out like walls. At Ches-
terton, one about eight inches thick had the gravel dug away on each
side for from twenty to thirty feet. Its sides were hard like mortar.
The direction was north and south. One at Barnwell, originally only .
a foot wide, after a few feet had been cut away terminated in the fault
shown in fig. 2.; and when a few feet more were cut down all trace
of disturbance was lost.

Fig. ye in the Barnwell Gravel-pit, showing a downward —
. slip or 6 wnches.

13 feet.

a. Marl bed. 6. Fine gravel. ce. Marl bed. d, Fine gravel.
The width of the faulted piece at the upper marl band is 7 feet.

These seem to me to be the typical facts of the Cambridgeshire
gravels; and it is only to be added that Prof. Hailstone and Mr.
Warburton, in an early volume of the Geological Society’s Transac-
tions, described the coarse gravel capping the Gogmagog and Harston
hills. From the Gogs, Prof. Sedgwick and I have collected exam-

1366. ] _ $EELEY—DRIFT OF THE FENLAND, 479

ples of nearly every rock in the north of England, especially those of
the Yorkshire coast (Kelloway rock, the sandstones, limestones, and
shales) and the Red Rock of Hunstanton. Though Carboniferous and
older Paleozoic rocks and fossils abound, and trap and plutonic rocks
are not rare, they are rounded boulders, the flints are often un-
broken, and there is a rough stratification. But the most important
fact about the deposit is, that descending on the east side towards
Fulbourn it becomes Boulder-clay *.

Part Il. TaHrorericat.
[ Abstract. ]

In this part of the paper the author endeavours, from, internal
and other evidence of the deposits, to indicate their origin and their
relative age.

1. Brown- or Boulder-Clay.—He concludes that, prior to the de-
pression of the country, when the Boulder-clay was formed, the Wash
had no existence, and that the Cretaceous barrier between Waynfleet
and Hunstanton was not broken through. He inclines to believe that
this Boulder-clay was deposited by drifting ice, on the hill-tops &c.,
much where now found, during a period of change so slow that the
fauna was able to migrate and follow it. There is no evidence in
the deposit of glacier-action ; but it contains rock-specimens such
as are now found in Yorkshire strata. It appears to be the oldest
drift-deposit of the district; and the author correlates it with the
Brown Clay or Till of the Norfolk coast.

2. Coarse Gravel.—tThis is chiefly found capping or bordering the
- Boulder-clay ; and the author infers, from its composition and rela-
tions, that it has resulted from the mud having been washed away from
the Boulder-clay during the period when the country was rising from
the sea. It is chiefly found on hills, and is of the age of the Con-
torted Drift of the Norfolk coast.

3. Deposits newer than the Fine Gravel of the Plains.—These are,
first, a Peat, anterior in date to the formation of Whittlesea Meer.
Under this is a Marine Clay with remains of Walrus, Seal, &c.,
Ostrea, Cardium, Scrobicularia.. It is named by the workmen
“buttery clay.” Under this is an older Peat containing extinct
mammals, suchas Bos frontosus, Bos priomigenius, Cervus megaceros.
Among the other species are Canis lupus, Castor europeus, Sus
scrofa, Cervus elaphus, Cervus capreolus, Lutra vulgaris, Ursus
arctos, &c. Among the fossils have been found teeth of Rhinoceros
and Hippopotamus, probably derived from the gravel. The fauna
of these beds is very similar to that of the newest gravel. They
correspond to the peat- and sand-beds which fill the valley of the
Mundesley Section.

* In a supplement to a Lecture on the Fens and their Fossils, Professor
Sedgwick (in 1862) gave a brief but clear account of these drift-deposits. I have
used Professor Sedgwick’s names as having the sanction of half a century of

teaching, and have freely availed myself of the Professor’s experience as given
in his Lectures. .

480 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

4, Fine Gravels of the Plains.—The author is of opinion that the
physical geography demonstrates these beds to have heen of marine
origin; and the false bedding is such as estuarine currents would pro-
duce. Hence itis inferred that these gravels were formed from denu-
dation of the Upper Chalk and local rocks, and of the coarse gravel and
old Boulder-clay. The presence of the marl-bed, composed largely
of Cretaceous foraminifera, shows by its fossils that since the period
of coarse gravel the country had become capable of supporting many
kinds of life. Reconstructed Boulder-clay and gravel must both
result from the same cause. The March deposit is regarded as the
oldest of the fen gravels, probably formed between the coarse gra-
vel and the marl-bed of the gravel of the plains.

These beds_are correlated with the Upper Boulder-clay and coarse
gravel of the Norfolk Section.

3. ADDITIONAL OpsERVATIONS on the GEoLoey of the LaxH-couNntTRY.
By Professor R. Harxwzss, F.R.S., F.G.S., and Henry Nicnor-
son, Esq. With a Nore on two New Srxcrzs of Triosrrus, by
J. W. Satter, Esq., F.G.S.

Recent investigations among the Skiddaw slates have made impor-
tant additions to the fauna of this portion of the Lower Silurian
series: the fossils which have been obtained have, for the most part,
come from the Coldale valley, from strata which form the lowest
rocks of the Lake-country*. There have now to be added to the
fossils of this portion of the Skiddaw slates two Trilobites, namely a
new form of Phacops, found at Whiteside, near Coldale, and Ayglina
binodosat. To these have to be added perfect tails of Caryocaris
Wrightit, the portion which had not been discovered when Mr. Sal-
ter’s figure was published; and these bear out in every respect the
sage dio. of this Crustacean by that paleontologist.

The lower beds of the Skiddaw slates have recently furnished other
fossils, among which is a small Lingula nearly allied to L. brevis,
Port., according to Mr. Davidson, and some small oval bodies
arranged in a ribbon-shaped form. These latter appear to be ova,
and they occur in the greatest quantities where Caryocaris Wrightit
abounds.

The branching Bryozoon figured in the Memoir referred to in the
note has also recently been met with in greater perfection among the
‘<Screes”” on the sides of Frozzengill. As figured in Mr. Salter’s
note, it is represented as small dichotomously branching stems.
The portions which have recently been obtained show stronger stems
than the original fossils, and these stronger stems have anastomosing
thinner portions, giving the fossil an aspect very like the corneous
axis of a Gorgonia.

* Quart. Journ. Geol. Soc. vol. xix. p. 116.
+ The latter, we learn from Mr. J. P. Morris, of Ulverston, was obtained from
Outerside, on the south of the Coldale valley, by Mr. Bolton.

1866. | HARKNESS AND NICHOLSON—-LAKE-COUNTRY. 4&1

The upper portion of the Skiddaw slates, which is more soft and
shaly than the middle and lower parts of the group, has also recently
furnished fossils which are new to this series in the north of Eng-
land. The locality yielding these fossils is not in the Lake-country
proper, but a spot in the north-east of Westmoreland. The twenty-
- first volume of the Quarterly Journal of the Geological Society, page
239, contains a section of the Lower Silurian rocks which occur im-
mediately west of the Pennine escarpment, showing the Skiddaw slates
rising from beneath the greenstones, porphyries, and ash-beds which
form Burney Hill. The Skiddaw slates here form an axis, the north
side of which is overlain by the greenstones, porphyries, and ash-beds
of Grumpley Hill; and immediately north of the axis, and cutting
through the Skiddaw slates, is Crowdundle Beck, into which a small
stream flows, which exposes a fine section of their higher beds. The
fossils which this section affords are principally Graptolites, among
which is Diplograpsus teretiusculus, a form not hitherto recognized in
the Skiddaw slates; and from this locality there has also been obtained
Agnostus Moret, Salter.

These additions to the fauna of the Skiddaw slates—a series of
deposits which was for a long time regarded as almost unfossiliferous
—although not large, are important, as they furnish for the first time
evidences of the existence of Trilobites and Brachiopoda in strata
which represent the Lower Llandeilo rocks in the north of England.

The thick series of greenstones, porphyries, and ash-beds which
in the Lake-country succeeds the Skiddaw slates, has hitherto yielded
no fossils, although the slaty ash-beds have been carefully examined
for them. ‘These newer rocks are the result of very different condi-
tions from those which gave rise to the Skiddaw slates, the latter
being purely sedimentary rocks, while the former were produced, either
directly (as in the case of the greenstones dnd porphyries) or indi-
rectly (in the state of ash-beds), by igneous causes. Notwithstanding
the difference in the origin of these two groups of Lower Silurian
rocks of the Lake-country, there does not appear to be sufficient
evidence to show that any unconformability exists between the Skid-
daw slates and the succeeding green rocks.

The band of Lower Silurian rocks which in Cumberland and
Westmoreland lies immediately west of the Pennine escarpment
contains, among the greenstones, porphyries, and ash-beds, a highly
fossiliferous zone, the strata forming which are dark flagegy rocks,
reposing on ash-beds which overlie the porphyry of Dufton Pike;
and this fossiliferous zone is succeeded by porphyry*. The igneous
rocks of this district bear great resemblance to those of the Lake-
country ; but the fossiliferous zone has a more decidedly sedimentary
aspect than any of the ash-beds which are associated with the green-
stones and porphyries of the latter area.

Notwithstanding this difference in mineral nature, there is in the
Lake-country a zone corresponding with the fossiliferous band of
North-east Westmoreland ; and it also affords fossils.

The porphyry which, among the Lower Silurian beds on the west

* Quart. Journ. Geol. Soc. vol. xxi. p. 242.

482 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

side of the Pennine escarpment, overlies the fossiliferous flaggy strata,
is succeeded by a limestone which is the equivalent of the Bala
Limestone of Wales, and of the Coniston Limestone of the Lake-
country. The Coniston Limestone of the Lake-country is well seen
in the valley of Long Sleddale, having been worked on both the east
and the west sides of the valley. To the north-west of this lime-
stone, and supporting it, is a porphyry agreeing in all respects
with that immediately beneath the Coniston Limestone of Keisley,
near Dufton, which separates the limestone from the fossiliferous
zone. In Long Sleddale, north-west of this porphyry are ash-beds
which have been worked for slates; but the quarries are now aban-
doned. The old slate-quarry is known as Style End Grassing Quarry,
and forms a portion of the southern skirts of Harterfell. Among
the débris of the quarry a few fossils may be obtained, which
make their appearance in consequence of some of the slaty rocks
weathering along the planes of bedding.

At Sunney Brow, a short distance west of Windermere Lake, the
same fossiliferous rocks occur, and under nearly the same circum-
stances as at Style End Grassing. A mass of porphyry here also
separates the ash-beds from the Coniston Limestone; and the ash-
beds have been worked for slates at Pull Scar, on the side of a hill
immediately north-west of Sunney Brow. The fossils are rare in
the slaty rocks, but they are by no means uncommon in the green
sandstones which interstratify the slaty beds of Pull Sear; and as
the coarser rocks have been used for diking, the fossils can be ob-
tained from the walls near the quarry, where they weather out
rapidly.

The fossils of Style End Grassing and Pull Scar are nearly iden-
tical. They consist of Stenopora fibrosa, Petraia subduplicata, Orthis
vespertilio, O. flabellulum, Strophomena tenuistriata, and crinoid
stems. The fossils of Pull Scar are less distorted by cleavage than
those of Style End Grassing, and in both localities the forms are
those which are most abundant in the fossiliferous flags of Dufton.
The coarser strata of Pull Scar resemble the fossiliferous ash-beds of
Snowdon ; the finer beds of Style End Grassing are nearly allied to
the ash-beds of Grange Hill, which underlie the Bala Limestone of
the Chair of Kildare, in both of which deposits fossils similar to those
of the ash-beds of the north of England occur.

The fossiliferous flags of Dufton, and the fossiliferous ash-beds of
the Lake-country, appertain to the Bala or Caradoc age. There
is, in the north of England, beneath these a great fucked of
igneous rocks, which separate them from the Skiddaw Slates, and
which probably represent the Upper Llandeilo group.

Although the evidence of the occurrence of the Upper Llandeilo
in the Lake- -country is not satisfactory, the Bala or Caradoc forma-
tion is well marked, and is capable of being divided into three dis-
tinct groups. The lower is made up of igneous rocks and ash-beds,
but has no well-defined base ; the middle consists of a mass of highly
fossiliferous limestone, with associated black shales, and has been
described by Professor Sedgwick under the name of Coniston Lime-

1866. | HARKNESS AND NICHOLSON—LAKE COUNTRY. 483

stone; and the upper portion is a series of dark-grey sedimentary
rocks, which, as it yields valuable flags, has been designated by
Professor Sedgwick the Coniston Flags. The higher portion of this
upper series is made up of coarser rocks, termed Coniston Grits by
Professor Sedgwick; and these form the top of the Lower Silurian
series of the Lake-country.

The fossils of the lower portion of the Bala or Caradoc group have
been already mentioned*. Those of the middle part of the series,
and also some of those of the upper portion, have been alluded to by
Professor Sedgwickt. Of the latter there occurs in an old flag-
quarry in Long Sleddale G'raptolites Ludensis ; and in the quarry now
wrought at Randy Pike, between Ambleside and Hawkshead, Pha-
cops obtusicaudatus, Salter, Orthoceras filosum, O. tenuistriatum, and
O. subannulatum are found.

The Coniston Flags, which are extensively worked at Broughton
Moor and Kirkby Iveleth Moor, afford additional fossils. These
consist of Diplograpsus pristis (which occurs in a high state of relief),
Orthis crispa, and Cardiola interrupta.

In the Furness district, to which Broughton Moor and Kirkby
Ireleth Moor belong, the three members of the Caradoc formation
are well represented, and they are the only Silurian rocks which
there occur. Their appearance in this district, to the exclusion of
other Silurian rocks, results from two faults, having north-east and
south-west directions, with downthrows towards the north-west.
These faults were alluded to by Professor Sedgwick at the Aberdeen
meeting of the British Association.

One of these faults crosses the country about two miles south of
Broughton in Furness, near Rake End, where the coarser beds of
the Upper Caradoc, the Coniston Grits, areseen. Immediately south
of Rake End is a mossy flat; and to the south of this flat, at Bank
End Hill, the Lower Caradoc appears in the form of porphyry. In
the mossy interspace the fault occurs. Southward from the porphyry
the Coniston Limestune is found, having been worked at Gill End
Gill, a short distance south-east of the village of Soutergate; and
south-east of the limestone the Coniston Flags again make their
appearance. A more southern fault, parallel to the one just alluded
to, occurs a little north of Dalton in Furness. This also brings
up on its south-east side the Coniston Limestone, which is seen at
High Haume.

Such are the two faults and their results; and had they been
traced north-eastward, they would have been found to extend beyond
the Furness district.

The Coniston Flags at Ross House, near Ulverston, afford Cardiola
unterrupta ; and the same rocks a little nearer Ulverston, at Games-
well, yield Actinocrinus pulcher greatly distorted by cleavage. The
fossils from these localities, and also those from Broughton Moor
and Kirkby Ireleth Moor, have been collected by Mr. J. P. Morris,
of Ulverston.

At Lowick, west of the Crake, which flows out of Coniston Lake,

* Toe. cit. supra, p. 248. + British Paleozoic Fossils, p. 356.

484 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [May 9,

Mr. Morris obtained from concretionary-limestone strata Orthis por-
cata, M‘Coy (O. inflata, Salter), one of the most abundant of the
Coniston-Limestone fossils; and to the south of this concretionary
limestone the Coniston Flags with Cardiola interrupta are again seen.
Still further south, “‘ at the south side of Tottlebank Fell, the Ireleth
limestone again appears, in the form of calcareous concretions ”
(Sedgwick, Letters on the Geology of the Lake-district). This Ire-
leth limestone is the Coniston Limestone, and at Tottlebank Fell it is
probably a continuation of the band seen at High Haume.

_ The repetition of the bands of Coniston Limestone shows that the
faults referred to by Professor Sedgwick extend at least as far as the
river Crake.

These limestone bands have not yet been detected north-east of
this stream; but the mineral character of the rocks which occupy
the country east of the Crake shows that they belong to the Conis-
ton Flags and Coniston Grits. The same rocks occupy the country
between Ulverston and Newby Bridge; and on-the eastern side of
Windermere Lake they form the Cartmel Fells. From these cireum-
stances, there is strong reason for inferring that the two faults inter-
sect the older Paleozoic rocks, from their south-west to their north-
east boundary.

The rocks occupying nearly the whole of the Lake-country ap-
pertain to the Lower Silurian series. There are, however, in the
south-east of this area rocks of a newer age, which are well exhibited
near Kendal. About three miles north-east of Kendal, near Shaw
End, is a quarry in the Upper Caradoc strata called Shepard’s
Quarry, which affords the same fossil as the rocks at Gameswell,
namely Actinocrinus pulcher. The strata here dip to the south-east,
which is the prevailing inclination of the Silurian strata of the north
of England.

To the south of Shepard’s Quarry is Benson Knot, the hill which
has afforded many Upper Silurian fossils ; and to the west of Shepard’s
Quarry is Potter Fell, where fossils similar to those of Benson Knot
occur; and in both these localities the fossils are widely different
from those of the Upper Caradoc group.

Two important members of the Silurian series are wanting in the
Lake-country, namely the Llandovery rocks and the Wenlock group.
In this district we have no smooth Pentamert; Atrypa hemaispheriea,
Encrinurus punctatus, and other Upper Llandovery fossils are ab-
sent ; nor do the characteristic fossils of the Wenlock group occur.

In the neighbourhood of Kendal the olive-coloured Ludlow rocks,
which abound in fossils, nowhere exhibit the strata on which they
repose. These Ludlow rocks seem to be brought abruptly against
the Upper Coniston group by faults; and to one of these is refer-
able the close proximity of the Coniston Flags of Shepard’s Quarry
and the Ludlow rocks of Benson Knot. This fault is probably a con-
tinuation of the more southern of the two faults which are so well
seen near Ulverston, and which have been traced north-eastward to
the Crake. Besides this fault, there is one, which runs west of
Shepard’s Quarry, and which also places the Ludlow rocks in contact

1866.] HARKNESS AND NICHOLSON—LAKE-COUNTRY. 485.

with the Upper Caradoc group ; this latter, however, has a different
course, and belongs to a different system of faults than those of
Furness.

There are in the Lake-country two distinct systems of faults:
but they are not confined to it; they occur in the north of England
wherever the older Palseozoic rocks present themselves, and they be-
long to different periods. The system which has a north-east and
south-west direction is older than the other; and an instance of the
occurrence of this system out of the Lake-country is seen in the
section from Melmerby to Roman Fell*. Here the fault brings in
eontact the Coniston Limestone and the Skiddaw Slates, the down-
throw being towards the north-west.

Another and a parallel fault was recognized last summer among
these old rocks of the north-east of Westmoreland, to the north-west
of that just referred to. It is seen along the course of a stream
which flows on the south side of Knock Pike, called Swindale Beck.
A short distance east of where this stream crosses the Pennine fault,
it flows over grey and purple shales; and among the former are
fossils similar to those of the flaggy beds of Dufton, but not in such
great abundance. Following the stream upwards, we have on its
south-east side Skiddaw slates, characterized by the branching Bry-
ozoon. Here, therefore, within two miles of the fault near Keisley,
we have a second downthrow of the rocks to the north-west, which
brings into contact the fossiliferous Lower Caradoc beds with the
higher portion of the Lower Llandeilo.

These north-east and south-west faults are of an ancient date.
They in no way affect the Upper Old Red Sandstone, which in some
spots rests unconformably on the older Paleozoic rocks of the north
of England; and the elevations and depressions which resulted from
the faults were entirely planed away before the period of the deposi-
tion of the Old Red Sandstone.

The second system of faults, which has nearly a north and south
course, is newer than the Carboniferous age, and was probably
produced even after the Permian epoch. One of the faults of this
system occurs among the rocks which in Cumberland and West-
moreland lie immediately west of the Pennine escarpmenty.

The faults of this system are very abundant in the Lake-country.
One of them traverses Windermere Lake and the country north
of it; and, passing along the valley in which Thirlmere is situated,
it continues onwards by Glenderattera, the valley separating Skiddaw
from Saddle-back, to near Overwater, where it brings the green rocks
of Binsey Crag, on the east, against the Skiddaw slates, which occupy
the comparatively flat country on the west of this hill.

Another of these faults, passing along the valley of the Duddon
northwards, intersects the rocks near Buttermere and Crummock-
water; and on the west side of the stream connecting these lakes
the Skiddaw slates can be seen in contact with the green rocks on
this line of fault.

* Quart. Journ. Geol. Soc. vol. xxi, p. 239.
+ Ibid. p. 246.

486 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

Along the lines of these newer faults the most important of the
English lakes occur; and they give to the Lake-country its bolder
features.

Some lakes, however, such as Hawswater and Wastwater, which
have a north-east and south-west course, occupy valleys which
appertain to the older system of faults. In the case of Ullswater
we have a more complex outline than usually belongs to the lakes
of the north of England. The first and lowest reach of the lake has
a north-east and south-west direction. At the south-west end of
this reach Hallan Crag presents a bold front, which results in part
from a fault running north and south, and crossing Ullswater from
the valley near Howtown. The middle reach of the lake commences
on the west side of the north and south fault; it also has a nearly
north-east and south-west direction, and terminates abruptly near the
north-western spur of Place Fell: the middle reach seems also to
occupy a valley produced by a fault belonging to the older system.

The upper reach runs nearly north and south. It occurs in a
valley produced by one of the newer faults, which, crossing Kirkstone
Pass, continues southward through Trout Beck ; and it is to one or the
other of these two systems of faults, or to their combined influence,
that the beauty of the Lake-country chiefly owes its origin.

Note on Two new Species of TRILOBITES.
By J. W. Satter, Esq., F.G.S.

1. PHacors NicHotsont, spec. nov. Figs. c & d.

There is too little of this species to enable me to give a proper
diagnosis. Itis evidently a species of the subgenus Acaste, and not
> distantly allied to P. Brongmarti,
a fossil from the Caradoc or Bala
rocks of Tyrone. I have two spe-
cimens—one found by Professor
Harkness, from which the figure is
taken; another, simaller, is in the
cabinet of Mr. H. Wyatt Edgell.
Each shows something the other
does not possess, and I shall de-
scribe them together, as the figure is a sketch made up from both
specimens.
The whole form is broadly oval, much depressed, about half an inch
wide, and about 1 inch long; the head is semicircular, rather pointed
in front, three-tenths of an inch long, and more than half an inch
wide. |
The glabella is trapezoidal, the sides are nearly straight and widel
diverging from the base, which is only half as wide as the forehead-
lobe. This is transverse, diamond-shaped, bluntly pointed, and
angular in front, and divided from the three lateral lobes by a slightly
sigmoid furrow, not deep, as in A. Brongniartii (the kindred species

1866. ] SALTER——-NEW SPECIES OF TRILOBITES. 487

quoted above), but neatly impressed and nearly reaching to the
centre. The upper lateral lobes are triangular, the middle transverse
and oval; the basal are linear, transverse, and nodose at the ends.
The neck-furrow is strong, and the neck-segment not broader than
the basal lobes.

The cheeks (imperfect) appear triangular, and are gently convex for —
a large space before reaching the very large curved eyes. These have
the eye-lobe linear and distinctly marked out; and the lentiferous
surface, broad and much arched, reaches from the termination of the
upper pair of furrows very nearly to the neck-furrow, which is rather
broad and well defined. We do not yet know the free cheeks: they
were probably short and mucronate.

The body-segments (seven are preserved in Professor Hark-
ness’s specimen) have a rather broad depressed axis, the rays being
obscurely nodular at the ends. The axial furrows are slight, and the
pleuree are flat as far as the remote fulcrum, which is placed halfway
out. They are deeply, but not widely, grooved to the very end of
the obtuse tips.

The pleure are bent down from the fulcrum, but not strongly,
unless the specimens are both compressed vertically (I think not),
and a little recurved.

Tail semicircular, convex only on the lateral lobes, which show
five straight long furrows directed a little backward, and as many
faint intervening ones. ‘The axis is moderately broad, conical, and
rounded at the tip, which reaches nearly to the end of the tail.

Locality.— Whiteside, three miles west of Braithwaite, Keswick.

2. Aenostus Moret, Salter. Figs. a & 0.

Ref. Decades Geol. Surv. xi. p. 7. pl. 1. f. 13, 1864.

In the Decade I was only able to give a figure of the head of
this most characteristic species, obtained by Mr. Lightbody and my-
self from the blacklead-bearing shales west of the Stiperstones,
Shropshire. |

It is an excellent proof that we are right in referring the Skiddaw
slates to the verge of these old Shropshire beds; so that the term
«« Arenig or Skiddaw group ” of Sedgwick is no longer a hypothetical
association, but indicates a definite horizon.

The head (it is figured at a from the Decade just quoted) is sub-
quadrate in outline; and the narrow bilobed and pointed glabella is
surrounded by a broad limb, deeply indented by numerous depressed
rays, interlined by shorter ones near the margin.

The tail, now figured (6), shows exactly the same ornament : nume-
rous (10 or 11) deep long depressions radiating over the limb, not
even, but nodose in their character, and interlined by smaller ones
toward the margin. The outline is quadrate, the border narrow,
except where it 1s produced into the short spines on the hinder edge ;
and these occur nearly as far back as the posterior margin. The
axis is about half the length of the tail, broad, short, pyramidal above,
soon cylindrical, and much flattened, marked across by two pairs of

VOL, XXII,—PART I, 21

488 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

furrows, which do not reach quite across; and there is some indica-
tion of an obtuse central tubercle.

Locality (of fig. 6).—Ellergill, near Milburn, Westmoreland. (In
the cabinet of Professor Harkness.)

4. On the Lowrr Sitvurian Rocks of the Istz of Man. By Pro-
fessor R. Harkness, F.R.S., F.G.S., and Henry Nicnotson, Esq.

Tue rocks which belong to the lower sedimentary series, and which
occupy the largest portion of the surface of the Isle of Man, have
been described by Dr. Berger*, and supplemental observations have
been made to his memoir by Professor Henslow 7.

The Rey. J. G. Cumming has also given a description of the old
rocks of the Isle of Man, with especial reference to the Carboniferous
Limestone of the islandt.

The older sedimentary rocks of the Isle of Man are also described
in Glover’s Guide to this island, which gives a condensed statement
of the memoirs of Dr. Berger and Professor Henslow§.

The nature and arrangement of the old rocks of the Isle of Man
are best seen in the coast-sections, which usually occur in the form
of bold cliffs. The interior of the island also affords sections in some
of the brook-courses ; but the mountains composed of these rocks,
which have usually a rounded outline, are covered to a considerable
thickness with soil and peat, which hide the rocky masses.

On the south-east side of the island, in the neighbourhood of
Douglas, good exposures of rocks are seen. Along the coast from
Douglas to about a mile north-east thereof, the strata appear in the
form of thin-bedded grey flags, having the mineral characters of the
Skiddaw slate, and dipping south-east at an angle of 60°. These
thin-bedded strata, on passing downwards, become thicker-bedded.
The rocks here are used for building-purposes, and the finer strata,
having a distinct cleavage, are to some extent used for slating.

The only trace of organic remains here is Palwochorda major, a
fossil very abundant in the Skiddaw slates of Cumberland.

- A short distance to the north-east, near the village of Onchan,
the same thin-bedded Skiddaw slates are seen; but a little to the
south-east of this village rocks of another character, consisting of
green slates and porphyries, make their appearance. These green
rocks form the headland called Bank’s Point, and they are well seen
at Crowdale on the east side of it. The green rocks and porphyries
which occur here are the equivalents of the ash-beds and porphyries
which succeed the Skiddaw slates of the Lake-country. They differ,
however, somewhat in their mineral nature from the rocks of the
latter country in being more quartzose and in having the ashy rocks
better bedded. These green rocks of the Isle of Man have the same

* Geol. Trans. vol. ii. p. 29 ef seg. t Geol. Trans. vol. v. p. 482 e¢ seg.

t Quart. Journ. Geol. Soc. vol. i. p. 317 e¢ seq.

§ The portion on the natural history, including the geology, of the Isle of Man
in Glover’s Guide was drawn up by the'late Edward Forbes.

1866. ] HARKNESS AND NICHOLSON—ISLE OF MAN. 489

dip and strike as the underlying Skiddaw slates; and they extend
north-eastward to near Clay Head, where the thin-bedded Skiddaw
slates again make their appearance.

The Skiddaw slates continue along the coast by Garwick to Laxey.
They are much contorted, but have a prevailing south-east dip.
North of Laxey, also, Skiddaw slates occur having south-east dips.
They are well seen on the high-road to Ramsey, about two miles
from Laxey, where a considerable cutting has been made through
them; and below this cutting, on the coast, they were formerly
worked for slating-purposes.

About half a mile beyond the cutting, and nearer Ramsey, granite
is seen on the roadside at a spot called Dhoon; and north of this,
about three miles from Laxey, on the road leading to Maughold
Head, the Skiddaw slates again appear, also with south-east dips.
A little north of this, and on the same road, at Regnabb, a granite
similar to that of Dhoon occurs. Further north, at Cornah, a hard
light-grey rock with no distinct bedding is seen, and at a short
distance to the north-west, at Marebreck, hematite has been worked
in the Skiddaw slates. About two miles north-east of Marebreck is
a bay on the south side of Maughold Head, called Porth Moar; and
in the north side of this bay the Skiddaw slates are well seen, dip-
ping north-west at 33°. Here they consist of hard flaggy rocks,
grey in colour. On the south side of this small bay the same hard
flagey Skiddaw slates occur with a south-east inclination. An anti-
clinal axis appears in the Skiddaw slates of Porth Moar; and inland
for some distance, either along or near this axis, hematite has been
wrought.

Section across the Isle of Man.

N.W. 8.E.
Orry’s Head. Greeba (1591 ft.). Douglas Head.

1

4
{
1
i]
o
.
\

a 5 ) 6b | e
a. Old Red Sandstone. 0. Skiddaw Slate. c. Green rocks (Ash-beds).

Maughold Head is composed of Skiddaw slates which dip north-
west ; and the same rocks and dip prevail along the road from Maug-
- hold Head to Ramsey, as far as Ballure.

At Ramsey, and in the country to the north, no rocks are seen,
Boulder-clay being the only substance exposed in this flat country ;
but to the west of Ramsey, as far as Sulby, the mountains, which
here rise abruptly from the Boulder-clay plain which forms the
northern portion of the island, exhibit exposures of the Skiddaw-
slate series. |

On the south side of the road leading from Ramsey to Peel, about
three miles from Ramsey, is a quarry where road-metal is now
worked. The bulk of the rock here is grey hard quartz-rock, with
occasional rounded pebbles of quartz imbedded therein. The quartz-

2, Tae

490 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 9,

rock here has a great affinity to the grey rocks of Cornah, which
have no distinct stratification. Here, however, black shales occur in
the quartz-rock, which dip at a high angle to the north-west.

The hills immediately south of Sulby, four miles and a half west
of Ramsey, have a distinct slaty nature, and the slates have been
worked for roofing-purposes. Here also the Skiddaw slates dip
towards the north-west. Along Sulby Glen, a narrow valley which
leads to the highest land in the island, good exposures of rocks occur ;
and here, too, the Skiddaw slates dip north-west. Over the col which
separates the Sulby River from the river Nib, rocks of the same age
occur; and among them the north-west inclinations obtain. These
rocks, with the same dip, continue to the river Peel.

From Peel the Skiddaw slates form the coast to Port Erin, and
have also north-west inclinations. At Glen May, about four miles
south of Peel, these Skiddaw slates have a conglomerate in them ;
and south of Glen May they abound in quartz veins. At Port Erin
the anticlinal axis which was seen as occurring at Porth Moar and
extending inland again appears; and on the south-east side of this
axis the strata assume the inclination shown among the Skiddaw
slates to the south of Porth Moar, namely towards the south-east.
The district around Castletown is principally occupied by Carboni-
ferous Limestone, which has been described by the Rev. J. 8S. Cum-
ming. About two miles east of Castletown, at Lang Ness, the
Skiddaw slates are again seen, being overlain on their edge by Old
Red Conglomerate. From Lang Ness north-eastward Carboniferous
Limestone again occurs, and forms the coast from Derby Haven to a
small stream about a mile and a half north-east, called the Santon
River. The Skiddaw slates reappear on the east side of this stream,
having south-east dips ; and with these dips they continue along the
coast to Greenwick, where they become coarser in their nature and
have a well-developed conglomerate in them like that of Glen May.
The Skiddaw slates continue onwards, forming the coast, somewhat
contorted but with predominant south-east dips, until Douglas Head
is reached. At Douglas Head a change takes place in the rocks,
green ash-beds making their appearance and conformably overlying
the Skiddaw slates. These ash-beds strike across Douglas Bay, and
include within them the Coniston Rocks, upon which the Tower of
Refuge is built ; and this strike connects the green rocks of Douglas
Head with those of Bank How. We consider the Lower Silurian
rocks of the Isle of Man to belong to the Skiddaw slates, the lower
portion of the green ash-beds and porphyries of the Lake-district
and the Lower Silurian rocks of this island being on the exact line
of strike of the Skiddaw slates of the Skiddaw country and of their
overlying green rocks.

The foregoing section, taken through the centre of the Isle of
Man, shows the position of the anticlinal axis which traverses the
island in a north-east and south-west direction, as it occurs near
the road leading from Douglas to Peel. The more mountainous
portion of the island lies on the north-west side of this axis. The
section also shows at its south-east end the ash-beds of Douglas

1866. ] HOLLAND—SINAI. 491

Head; and at its north-west extremity the Old Red Sandstone,
in the neighbourhood of Peel, coming against the Skiddaw slates.

May 23, 1866.
The following communications were read :—

1. Notes on the Grotoey of Srna.
By the Rev. F. W. Horzanp, M.A.

{Communicated by Sir R. I. Murchison, Bart., K.C.B., F.G.S.]
(Abstract. )

THE peninsula of Sinai may be divided into three geological districts,
named from the granitic, limestone, and sandstone rocks of which
they are composed.

The whole of the northern portion of the peninsula is occupied
by an extensive plateau of limestone, supported on the south by the
range of Jebel-et-Tyh, and sloping gradually towards the Mediterra-
nean Sea.

A broad belt of sand, called the Debbet-er-Ramleh, separates this
limestone from the southern portion of the peninsula—although
small patches of it, apparently underlying the sandstone, are found
further south in Wady Badera and Wady Mokatteb, and in the
neighbourhood of Jebel Hummam, and also on the north-west of
Jebel Serbal, there occur large tracts of a limestone more cretaceous
in its character, and abounding with bands of flints. At the latter
spot I observed one mountain of Nummulitic limestone; and a
limestone of more recent formation, which abounds with fossils,
occurs near Tor and Ras Mohammed.

The granitic district forms, as it were, the backbone of the southern
portion of the peninsula. Its mountains are frequently seamed from
top to bottom with veins of porphyry, greenstone, and basalt, which
give them a peculiar striped appearance ; this is especially remark-
able on the east of Wady Mokatteb, the north-west of Jebel Serbal,
and in the wadies between Jebel Musa and Ain Hudera. They are
also in some parts capped by a stratum of sandstone of considerable
thickness and perfectly horizontal stratification, proving that an
enormous denudation has taken place. Both the limestone and sand-
stone, when found in close proximity to the granitic rocks, exhibit no
change in their structure; and thus, as well as by their uniform
horizontal stratification, they show that they must have been depo-
sited subsequently to the upheaval of the latter. The only traces of
active volcanic agency which are now to be found in the peninsula
are the boiling sulphur-springs and hot caves at Jebel Hummam, and
the two warm mineral springs near Tor. The mountains of the
granitic district appear to be chiefly composed of syenite; but
granite, porphyry, gneiss, mica-schist, and quartzose and horn-
blendie rocks occur in many localities. I did not succeed in finding
any traces of metallic ores in this district.

492 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

The sandstone formation appears to have formed the great mining-
district of the ancient Egyptians in Sinai. The principal places
where this formation occurs are Serabit-el-Kadim, Wady Mughara
and the south of Wady Mokatteb, the west of Serbal, and the neigh-
bourhood of Ain Hudera. The sandstone is generally of a reddish
ferruginous colour, though its surface is for the most part coated with
a dark-brown oxide of iron. The principal Egyptian mines were
apparently turquoise-mines, not copper-mines as has been generally
supposed. Serabit-el-Kadim and Wady Mughara were the chief
stations. The turquoises appear to be distributed more or less in
veins, though their occurrence is very uncertain ; and Major Mac-
donald, who has been working the mines for several years, has
often spent weeks with no success, and then suddenly found a large
number together.

I do not believe that any traces of copper are to be found either
at Wady Mughara, or Serabit-el-Kadim, excepting at the latter place
a thin film of silicate, too small, however, in extent for any practical
purpose. The specimens which I have brought from the supposed
slag-heaps on either side of the ruined temple on the summit of
Serabit-el-Kadim prove most clearly that they are not slag-heaps
at all, but merely a natural impure ore of iron and manganese. The
siliceous brown iron-ore, however, which abounds near Wady Mokatteb
and Wady Mughara, seems to have been extensively worked both by
the Egyptians and also, perhaps, by a less-civilized race after their
time ; and stone hammers, and flakes of worked flint are frequently
found on the mountain-sides.

At ashort distance from the mouth of Wady Shellal, on its south-
ern side, Major Macdonald has discovered a large heap of undoubted
copper-slag, which still retains a considerable quantity of copper in
it. I also obtained a small specimen of a rock containing a very
large proportion of carbonate of copper, and some pieces of malachite;
but I could not discover the locality whence they had been procured.
The sandstone abounds with salt and natron, and the water obtained
from itis always more or less brackish. In some of the wadies con-
siderable beds of curiously crystallized salt are found. From the
limestone I collected several specimens of fossils, consisting chiefly
of Echinodermata and EHxogyre; but in the sandstone I found but
one organism, a portion of the stem of a fossil plant. A consider-
able elevation of the western coast of the peninsula has apparently
taken place. A few miles to the north of Tor, large quantities of
shells in a semifossil state, but similar to the existing species, are
found at a height of 20 to 30 feet above the present level of the
sea, and large blocks of coral occur at a still higher elevation ;
considerable raised beaches also occur at Ras Mohammed. Yet Ido
not suppose that any extensive elevation of the land at the head of
the Gulf of Suez has taken place in modern days; nor does it appear
from the formation of the. ridge of Chalouf-et-Terraba, which
separates the Bitter Lakes from the Red Sea, that the two were ever
naturally connected, except indeed it were in prehistoric times.

Of the agencies which are still at work in modifying the surface

1866. ] WOODWARD-——OLDEST BRITISH CRAB. 493

of the country at the present day, frost and rain appear to play the
most important part in the higher mountains of the granitic district;
but the chemical action of the atmosphere seems to affect to a greater
degree the sandstone, by destroying the ferruginous cement which
binds together its particles, and thus decomposing it. Yet the
changes that are taking place are apparently so gradual and slow,
that I feel convinced that the peninsula of Sinai is to this day but
little altered in its nature from what it was when the children of
Israel wandered in its wilderness more than 3500 years ago.

2. On the oldest known British Cras (Paleinachus longipes) from
the Forust Marsiz, Matmespury, Wits. By Henry Woop-
wARD, Hsq., F.G.S., F.Z.S. (of the British Museum).

[Puate XXTV. fig. 1.]

I am indebted to my friend Professor Thomas Bell, F.R.S., of the
Wakes, Selborne, Hants, for the opportunity of describing this new
and beautiful crustacean.

The specimen is from the Forest Marble of Malmesbury, and was
discovered several years ago by the well-known collector of Oxford-
Clay and Oolitic fossils, Mr. Wm. Buy. It will be seen to have nearly
all its limbs zm situ; and it shows the carapace with four segments of
the abdomen united to it, resting upon a slab of Forest Marble covered
with the remains of Pentacrini, Acrosalenia hemicidaroides, shells of
Avicula, Rhynchonella, and traces of the drift-wood to which the
Oolitic Pentacrinites (like the barnacles of our modern seas) were
attached.

The limbs of this. crustacean are extremely long and slen-
der; and in this respect, and also in their form and in that of
the carapace, with its remarkable prominent tubercles in front, it
closely resembles the common “ Spider Crabs” (the Maiade and
Leptopodide) living on our own coasts at the present day, and the
Great Japanese Crab, the Inachus Kempferi, of De Haan. The Upper
White Jura of Germany has yielded carapaces of several minute
erustacea, which are either Brachyurous or Anomurous; but as no
limbs or abdominal segments have been met with, it is more doubt-
ful where to place them in a classification of the fossil forms.

Professor Reuss* and H. von Meyer?+ have described three genera
and twenty-five species of these forms (some of which have been re-
produced in Mr. Lowry’s ‘ Chart of Fossil Crustacea ’t); but none of
them are comparable with the carapace of Palwinachus.

* Sitzungsb. K. Akad. d. Wiss. in Wien, xxxi., 1858.

+ Palzontogr. Cassel, 1859-61, Bd. vii. p. 183, t. 23 (Monograph on the
Prosoponide),.

t Paleinachus longipes is there figured with the generic name Protocarcinus
which had been given to it (in MS.) by Prof. Bell; but it is not adopted here,
first, because the fossil has no affinity to Carcinus, and secondly, because the
prefix “ Proto” is objectionable in Paleontology.

494 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

In the swollen form of the branchial regions, and the well-
marked nuchal furrow, it resembles the genus /nachus, with which
it also agrees in the form and proportion of its limbs; but the bifid
and diverging rostral tubercles more nearly agree with the Maiade,
thus offering a connecting link for these divisions of Milne-Edwards’s
Triangulares. The Triangular Crabs are certainly one of the
earliest families of Brachyura; and notwithstanding their dull
habits, they make up by their exceeding fecundity* for want of
strength and cunning, and have thus been enabled to maintain their
ground even to the present day.

PaLminacuvs tonerpes, H.W. Pl. XXIV. fig. 1.

Carapace suborbicular, broadest behind; branchial regions large
and rounded, their surfaces covered with extremely minute rounded
tubercles; the gastric region well defined by a somewhat deep
furrow ; the frontal and hepatic regions more than half the length
of the entire carapace, tumid and ornamented with two subcentral
tubercles and a semicircle of five other tubercles ; margin irregularly
swollen and depressed, and contracting towards the rostrum, which
is represented by two prominent widely diverging and rounded
horns, at the exterior bases of which, in the recent Leptopodide,
the eyes are placed; these, however, cannot be detected in the
fossil.

The abdomen is imperfect, but indicates a female; the lateral mar-
gins of the most perfect segment are somewhat angular, deeply grooved
across, and also between the central portion and the epimera.

The arm, wrist, and hand have respectively five, three, and two
tubercles on their upper angle; the hand is didactyle, and resembles
the recent Stenorhynchus in form.

The walking legs are of about three times the length of the
carapace, very slender, and have a row of minute tubercles upon
their upper surface.

Breadth of carapace across the branchial region 8 lines, length from
attachment of abdomen to base of rostral spines 9 lines; rostral
spines 22 lines in length ; arm about 5 lines; wrist 23 lines; hand
53 lines; longest limb 28 lines.

EXPLANATION OF PLATE XXIV. fig. 1.

Fig. 1. Paleinachus longipes, H. Woodw. Forest Marble, Malmesbury, Wilts.
atural size.

————

3. Notes on the Spxcies of the Gunus Eryon, Desm., from the
Lias and Ooxrre of Enetany and Bavaria. By Henry Woop-
WARD, Hsq., F.G.S., F.Z.8. (of the British Museum).

[Puates XXIV. figs. 2-4, & XXV. figs. 1-3.]
Tur genus Hryon was established by Desmarest (in Brongniart
and Desmarest’s ‘ Natural History of Fossil Crustacea :’ Paris, 1822)

* The female Maia sqguinado bears at one time upwards of seventy-six
thousand eggs (Couch).

1866. ] WOODWARD—ERYON. 495

for certain forms of Astacide, with extremely broad and flat cara-
paces, found in the Lithographic stone of Solenhofen, one of the
earliest known geological localities on the continent, and perhaps
the most prolific in its yield of organic remains.

Only one species was then determined—the Eryon Cuviert of
Desmarest (Macrourites arctiformis of Schlotheim (1820), Locusta
marina of Bajer (1757), and first figured by Knorr and Walch
in 1755). Since that time Herr Germar, Count Minster, H. von
Meyer, Professors M‘Coy and Quenstedt have each contributed new
species. Lastly, the late Dr. Albert Oppel, of the Royal Bavarian
Museum, Munich, a Foreign Correspondent of this Society (whose
early death we must all lament*), has collected, revised, and added
to our knowledge of this genus, so that in 1862 (the date of his
book) the list of recorded species amounted to fourteen +.

Professor M‘Coy was the first to record an English species of this
genus, the Hryon Barrovensis, from the Lias of Barrow-on-Soar,
Leicestershire. [See the ‘Annals and Magazine of Natural His-
tory,’ 1849, p.172.|] But as his description varies in some points
and is unaccompanied by a figure, I have ventured to delineate it
by the help of the fine examples in the cabinet of the Rev. P. B.
Brodie, F.G.S., and those in the British Museum. I also subjoin a
revised description of it, and notices of other British species of this
genus from the Lias and Oolite, collected and lent by Charles
Moore, Esq., F.G.8., of Bath, Captain Hussey, of Lyme Regis, and
from specimens in the British Museum obtained by E. C. H. Day,
Esq., F.G.S., formerly of Charmouth.

Eryon, Desmar. 1822.

Coleia, Broderip, 1835, Trans. Geol. Soc. 2nd ser. vol. v. t. 12.
oe Bae

1. Eryow antiauvs, Brodp., sp.

Although unwilling to abolish a genus named in honour of so
great a geologist as the Karl of Enniskillen, I am compelled to
endorse the decision of my late friend Dr. Albert Oppel, and make
this the first and largest English species of the genus Eryon (EHryon
antiquus, Brodp. sp.)t.

From the Lias, Lyme Regis.

2. Eryon Barrovensis, M‘Coy, 1849. Pl. XXYV. fig. 1.

The carapace of this species (like that of its congeners) is extremely
flat, about one-eighth broader than long, the posterior margin is
truncated, the lateral margins are fringed with minute spines ; two
indentations intersect the border on either side (the first being some-
. what behind, and the second upon the line of the cervical furrow),
and enclose between them a short rotundato-quadrate lobe.

* Dr. Oppel died on 22nd December, 1865, at the early age of thirty-four
years.

t Vide Palaontologische Mittheilungen aus dem Museum des Kon. Bayer.
Staates, von Dr. Albert Oppel : Stuttgardt, 1864.

t See Oppel’s Pal. Mittheil. p. 11.

496 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

The sides of the carapace curve rapidly inwards in front, leaving
the anterior margin only half the width of the posterior portion.

The carapace is broadly notched in front with two lateral orbital
fossee formed by the lateral angles of the carapace.

A tuberculated ridge passes up the centre of the carapace, from
the posterior margin to the cervical furrow, by which it is inter-
sected ; it reappears for a short space in front.

Two lateral equidistant tuberculated ridges mark out the branchial
regions, and are also continued smoothly upon the frontal portion of
the carapace. :

Kach antenna of the inner pair has two many-jointed sete, the
outer one being slightly the longer. Each of the outer antenne
has a large oval scale attached to its broad basal joint; the sete are
single, and scarcely thicker than those of the inner pair.

The eyes, but rarely preserved, are placed near the base of the
scale of the outer antenne. In a specimen from Lyme Regis (from
Mr. Day’s collection, and now in the British Museum) the external
pair of footjaws (or sixth pair of maxillary appendages), with their
broad oblong basal joints and their more slender four-jointed palpi,
are well preserved.

The first pair of legs are robust and short, as compared with
Eryon antiquus, the hand and carpus nearly equalling the length of
the middle of the carapace; fingers slender, pointed, of equal length,
incurved at the tip, the moveable one most incurved.

The succeeding pairs of feet are much smaller, and are each ter-
minated with pincers, except the fifth pair, which are monodactylous
at their extremities. The abdomen is slightly longer than the cara-
pace, and one-third less in width; the first segment is narrow, and
has two tubercles on its lateral margins; the second, third, and
fourth have each two lateral and a median tubercle ; the sixth seg-_
ment has a median and two lateral ridges; these are continued on
the seventh segment or ‘telson,’ which is acutely triangular in
form; the caudal plates are very broad, and roundly quadrate in
form; the outer pair of plates are divided by a curved suture near
their extremities as in other Astacide*.

The epimera of the first five segments are rounded; that of the
sixth is faleate, and to its lateral and posterior margins the caudal
lamelle are articulated.

Dimensions (from a specimen in the British Museum).—Length
42 inches ; extreme breadth of carapace 2 inches 4 lines; length
of carapace 2 inches 2 lines; breadth of frontal portion of carapace
1 inch; length of abdomen 2 inches 8 lines, breadth of same 13
inch ; breadth of caudal plates 2 inches 4 lines; extreme length
of chelee 2 inches 10 lines (length of second pair of limbs 2 inches
4 lines, Mr. Brodie’s specimen) ; breadth of first pair of limbs .3
lines, second pair 2 lines.

Localities —Lias, Barrow-on-Soar.

The affinities of this species are more with Hryon antiquus, save

* This suture is absent in the outer caudal lamellz of the Solenhofen species
—a most important distinction: they differ widely also in form.

— :1866.] WOODWARD—ERYON. 497

for the extreme length of the forearms of the latter and the more
oval form of its carapace.

3. ERyoN CRASSICHELIS, spec. nov. Pl. XXV. fig. 2.

I have had the opportunity of examining two specimens repre-
senting this species,—one a detached and folded carapace, exhibiting
the upper surface ; the other an almost entire example exhibiting
the under surface—a position in which at least nine-tenths of the
specimens occur, not only in our own Lias, but in the Lithographic
Stone of Solenhofen.

The separate carapace (obtained by Mr. E. C. H. Day, F.GS.,
and now in the British Museum) is one-third broader than long,
and is altogether more rounded in form than #. Barrovensis or
EL. antiquus.

The branchial margin has along its border a row of strong spines,
which gradually decrease in size towards the frontal portion of the
carapace, where they entirely disappear.

The indentations along the lateral margins of the carapace are
less deep, and the lobes formed thereby have not the pointed cha-
racter seen in #. Barrovensis and other species. The orbital fosse
are rounder, and have one spine on their exterior border ; the rostral
notch is but slightly indented.

Between the orbital fossee and the nuchal furrow there is seen
upon the margin of Mr. Day’s specimen a prominent round body,
which, from its form, is most probably the eye somewhat displaced ;
but in £. arctiformis they are placed outside the outer antenne.

The surface of the carapace is uniformly and finely punctated,
and has the three ridges seen in Hryon Barrovensis; but they are
not tuberculated, save at the posterior margin, where one tubercle is
placed at the base of each of the lateral ridges.

A striking distinction marks this species, in the shortness and
thickness of the hands (as seen in an almost entire example from the
collection of Captain Hussey of Lyme Regis). The fixed and move-
able digits are less equal, broader, and more curved than in the other
English species.

The four following pairs of limbs are only imperfectly preserved ;
nor does the underside of the abdomen yield much detail.

The seventh segment (or telson) is perhaps more pointed, and the
caudal plates less round, than in £. Barrovensis.

The only species with which I am acquainted that is furnished
with hands like FE. crassichelis 1s the EH. Escherv*, Oppel (also from
the Lower Lias); but the specimen is one-half the size and too
imperfect for comparison, save in the chele. The specimen figured
by Oppel is from Miulligen, near Baden.

Dimensions.—Carapace (detached) : length 2 inches 1 line ; breadth
3 inches (measured across the branchial region); breadth of frontal
portion of carapace 16 lines.

Nearly entire specimen (Captain Hussey’s collection) :—Greatest
length of animal 3 inches 6 lines; greatest breadth of carapace 1

* See Oppel, op. czz. t. 1. fig. 1, p. 10.

498 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

inch 10 lines; greatest breadth of abdomen 1 inch 1 line; length of
carapace 1 inch 7 lines; length of abdomen 1 inch 10 lines; length
of telson 7 lines; length of forearm and hand 15 lines; breadth of
hand 4 lines.

4, Eryon WILMCOTENSIS, spec. nov. Pl. XXIV. fig. 3.

A slab from the collection of Charles Moore, Esq., F.G.S., of Bath,
contains no fewer than fifteen individuals of a small species* of Eryon,
which I have been extremely unwilling to treat as distinct from £.
Barrovensis, on account of the circumstance that the entire group are
preserved with their ventral surfaces exposed, and in none can the
contour of the carapace be traced.

Among the specimens from the collection of R. F. Tomes, Esq.,
F.Z.8., is a small carapace without any appendages, which, how-
ever, agrees very well in size with the above-mentioned examples,
and may, perhaps, be identical with them.

The former is from the railway-cutting at Pyle Hill, near Bristol,
from the “insect-bed ” or “* Modiola-minima”’ bed of the geological
surveyors, one of the basement beds of the Lower Lias.

The latter is from Wilmcote, near Stratford-on-Avon, from the
“<bottom block ”-bed of the Lower Lias.

This carapace (see figure) is somewhat shorter and broader in its
proportions than ££. Barrovensis (measuring 143 lines in breadth,
12 lines in length); the branchial region is more rounded ; and the
dentations around the margin of the carapace are much wider in
proportion to its size; whilst the relative distance across the frontal
portion is twice that of #. Barrovensis. ‘The surface of the carapace
is evenly covered with minute granulations ; and there are no large
tubercles along the median line, such as occur in the former species.

Whether the Pyle-Hill specimens be identical with the Wilmcote
example remains to be proven; in the meantime I have ventured to
name the carapace Walmcotensis, as I think it important to draw
the attention of Liassic paleontologists to this subject, in the hope
that more complete specimens may be sought for.

5. Eryon Bropret, spec.nov.t Pl. XXIV. fig. 2.

This unique form is from the Lower Lias rock, Lyme Regis, and
is at once distinguishable from the other species of this genus by its
more strongly ridged carapace and the straightness of the margin
along its branchial regions; the greatest width of the carapace is not
in the centre of the branchial portion, but at its extreme front, from
which point the breadth decreases to one-third at the posterior mar-
gin, which, however, is mutilated. The hepatic region is less dilated
laterally, but wider in front than in #. Barrovensis ; and the orbital
fossee and rostral indentation are less deep. In this specimen one
eye is preserved am situ. A second furrow (but faintly seen in the
centre of other species of Hryon) crosses the entire breadth of the

* Measuring 2 inches in their greatest length, and about 3 inch in width.
t British Museum Collection.

1866. | WOODWARD—ERYON. 499

carapace behind the nuchal furrow, entering the margin at the latero-
posterior indentation.

A rounded protuberance occupies the centre of the carapace in
front of the nuchal furrow, and a small tubercle behind it. There
are two lateral furrows upon the branchial region on either side of
the mesial ridge. The surface of the carapace is sparingly granu-
lated. }

Dimensions. — Length of carapace 2 inches (when perfect) ;
greatest breadth 1 inch 10 lines; width in front 11 lines; width
at nuchal furrow 1 inch 4 lines.

I have named this example after the president of the Warwick-
shire Naturalists’ Field-club, the Rev. P. B. Brodie, M.A., F.G.S.,
who has obligingly placed his collection at my service.

6. Eryon Moore, spec. nov. Pl. XXV. fig. 3.

Those who have visited the Bath Museum (especially during the
British Association Meeting in Bath) will remember the fine suite of
fossils from the Upper Lias fish-bed obtained by Mr. Charles Moore,
F.G.S., of Bath, who has devoted years of labour to the investigation
of this and other Jurassic beds.

Among a number of specimens (including six or seven different
species) is the present very perfect little Hryon, which I have named
after its discoverer.

The original is 14 lines in length, and 6 lines in its greatest
width. |

The carapace is smooth and nearly oval, but truncated at its
extremities, being 4 lines wide at its posterior border, and 23 lines
at its anterior.

A double furrow, uniting in the centre of the carapace, crosses
the entire breadth, diverging at the lateral border, and forming, by
two slight indentations, a square central lobe on either side, 1 line
in breadth.

A small projecting tooth marks the shallow orbital depression
on either side, while two prominent rostral spines enclose the
antenne.

The forearm (which is the only limb preserved) is, in its entire
length, equal to the length of the carapace, of which the slender
didactyle extremities form one fourth part.

The median ridge of the carapace only extends as far as the
nuchal furrow. '

The frontal central portion is tumid, and is slightly granular
anteriorly. —

The abdominal segments are 4 lines in width, and are strongly
grooved transversely, and have their lateral margins granulated.

The telson is acutely angular; the side lobes are more narrow and
pointed than in the other English species, more closely resembling
in this respect H. arctiformis from Solenhofen.

Eryon Moore is represented in the Solenhofen Stone by £. Schu-
berti of Meyer, from which it differs, however, in the lateral emargi-
nations and transverse furrows on the carapace, HL. Schuberti being

500 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

apparently destitute of a nuchal furrow; it differs also in the form
of the anterior border of its carapace.

Upper White Lias. Ilminster. Museum of Charles Moore, Esq.,
F.G.S.

7. Eryon OppeEtt, spec. nov. Pl. XXIV. fig. 4.

I beg leave to call attention to a curious specimen of Hryon (part
of the Hiberlein collection, now lodged in the British Museum)
from the Lithographic Stone of Solenhofen.

It is preserved upon the plane surface of a slab, and shows the
five pairs of limbs, the large and broad maxillipedes with their palpi
attached, one of the inner antenne with its two sete, and, lastly,
the fourth, fifth, sixth, and seventh abdominal segments with their
caudal plates attached.

Out of the large number of specimens of Hryon which I have
been able to examine from Solenhofen, and among the numerous
examples figured, I cannot find a single instance in which, as in
this individual, the first pair of chele are so small as compared with
the four succeeding pairs of legs, or in which the caudal plates,
including the central plate (the telson) are so remarkably round and
broad.

In illustration of the complete manner in which the Solenhofen
Crustacea have been treated, I believe this to be the only inde-
terminable example out of a collection containing upwards of 400
specimens of this class.

I propose to name it Hryon Oppeli, after the author of the
‘Palaontologischen Mittheilungen,’ whose works will long remain
his best monument.

Length of forearm 1 inch 4 lines, breadth 2 lines; length of
chele 2 lines, second pair 18 lines long, breadth 13 line; length
of third pair 14 lines, breadth 13 line; length of fourth pair 13
lines, breadth 14 line; all these are chelate, but the fifth pair are
monodactylous; length of fifth pair 74 lines, breadth 1 line.

Maxille 54 lines in length by 3 lines in breadth, semiorbicular
in form exteriorly, interior margins straight and finely serrated ;
palpus 3 lines in length; antenne 34 lines in length; abdomen
84 lines in breadth; telson 7 lines long by 64 broad—with the
overlapping caudal plates, making 11 lines in breadth.

Eryon, sp. ?

I wish to record the fact that Mr. Moore has also obtained from
this same Upper Lias rock a fine Hryon, which measured at least
6 inches in length, its abdomen 2 inches in breadth, and the cara-
pace probably 23 inches; much of the latter, however, has been
destroyed; and therefore I do not feel warranted in giving it a
specific name, as it may perhaps prove to be Hryon antiquus when
we know more about it.

Eryon, sp?
Lower Chalk, Steyning. (Vide Morris’s Catalogue, p. 108.)
This is probably a portion of a Squalla, several fragments of which

1866.] WOODWARD—ERYON. 501

have been found. Two are in the British Museum (from Mrs.
Smith’s collection), from the hard chalk of Dover; another is in the
collection of James Carter, Esq., of Cambridge, and is figured in Mr.
Lowry’s ‘Chart of Fossil Crustacea.’ I know of no Cretaceous
species of Hryon.

Lias. Dogger. |Malm
Sat
BE
ElS/ Bele] lal ela
B/S/PIS/S/PIM/o]4
Eryon, Desmar.
MPPMEOpINGUUS, SCHIOL. 0. ce oe ca se cece ee ce ees las %
mune PRUDUIE ENS GCP I awit kde tratole clap tiers ef tierere esiaiwiforer|'s oi oof ef oe *
POMCUPIRIC URLS: MIGU0SI% oss svete ie slat sid are bie ee aie/is [ais] sie eds ole | %
Pee SHES, LH ISEbao 5 shins inna Biesd alana aielaa |e | ois .| *
PETETPOEIIG: SCHIOU. aie soins cvs as Son acecgaue nce’ | %
REMERON ICTS! ce ga cover Fn oe ed pee mele cle elaales tw esia ets als «|
ce LEDS SESE il CSI OnE SR aang Rd Saray | ed ear ee ot a *
em Ele, CIS ars few 'e Eo. Sascha nti ee Scioto nell Sete ae ala dial tay
9. Redenbacheri, Miinst. . Bi sa Paps es “athens eeadl a ua Mlicbertieasel cdl mv dlcyedl toed ed [ade
10. Perroni, Efall... hedges aerate ears ve eae eae oot ae, | etnies [eailavclters tom ese
11. Hartmanni, Meyer — Be TRE hte aere ete epee Pe. ote) ster sca
MSUIAPOSNY, “THOTCCTO. 0.5 wn cee ee abe ec ee ele eles %
PI IAL ota Pasa. vs oye) Sor ere oreh owiccn ele wie a's *
LOL CLUE C NTS e720, a x
esarrovensis, Coy 2... 8. cc ee ee ne cee ae te *
MeammINPoumet 27) WV OOUU, . 5... as be a oe tes wceree woleotes *
Pee aimeotensis, 7. Woodw. :.-. 06.0 cc ce ca es *
He IOl FF. WVGORW. Five ee eae pale stele we ve *
tarerpesiehelis, JF, Wood. ic. cece eee gee yess *
SPMD EP AY OOO ID. So. oop 3p 0,0 in eset «gaya ~ anainssveiasellin ail 4%) .sife il ore fn eadsilin ad
6 3 1 |10

Nors.—The species, in the above Table, numbered | to 9 are from the Solen-
hofen Limestone, and described and figured by Dr. Oppel (op. ci¢.), also :—
_E. Escheri from the Lower Lias, Baden.
E. (Coleia) antiquus, Lower Lias, Lyme: by Mr. Broderip, Trans. Geol. Soc.
2nd series, vol. v. t. 12. f. 1 & 2.
E. Barrovensis, Lower Lias, Barrow-on-Soar: by Prof. M‘Coy, Ann. Nat. Hist.
1849, p. 17 2.
ae eeienanni: from the Upper Lias, Wirtemberg: by H. von Meyer, Nova
Act. Acad. C. xviii. Bd. p. 263.
E. Perroni, from the Oxfordian, Calmoutiers, Haute-Sadne, France: by M.
Etallon, Crust. Foss. de la H.-Sadne, Bullet. Soc. Géol. de France, t. xvi.
p. 169, tab. 4. f. 1-3.
E. Edwardsii, from the Upper Lias, Calvados: by M. Moriére, 1864, Bull. de
la Soc. Linn. de Normandie, t. viii. p. 89, pl. vi.

For directing my attention to this last species, I am much indebted to
Mr. Ralph Tate, F.G.S., the obliging Subcurator of the Geological Society’s
Museum.

The remaining five species enumerated are figured and described in this paper.

Although the genus Hryon occurs fossil at Solenhofen with a
Iimulus so like our own recent species that, I think, no one will

502 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

doubt their consanguinity, yet the former has died out, and the
latter remains to this day.

The Scyllaride, which take their place at the present day, have
only a mimetic resemblance to them, the simulation being assisted
in a great degree by the broad scale-like form of the outer pair of
antenns, which are flattened out and le in a plane with the cara-
pace. They, however, offer some points for comparison, and occur
most commonly in the China Seas and on the coast of Japan, asso-
ciated with recent Zimuli and forms of Palinurus, &c., which are.
found together in a fossil condition in Bavaria.

Where a series of similar forms occur together, fossil and recent,
it is fair to infer a similarity of conditions favourable to such a
group.

The wide tracks of fine argillaceous mud which characterize th
enormous rivers of China, the coast, and its adjacent islands, agree
well with the lithological texture of the Solenhofen beds in which
the fossil crustacea le imbedded; and the terrestrial conditions
evidenced by the remains of Sauria, the Archwopteryx, and Ptero-
dactyles, with countless Libellule, spiders, and Cycadee of large size,
point to a continent close at hand, the rivers of which brought down
the periodic mud-avalanches which entombed the cuttlefishes and
crustacea in such quantities both at Pappenheim and Solenhofen.

By referring to the preceding Table, it will be seen that only three
continental species of Hryon (H. Escheri, Hdwardsi, and Hartmannt)
occur in the Lias, the remainder being from the Lithographic Stone
(Upper Oolite).

We ought then, I think, either to find many more species in our
Oolite, or to regard the lithographic species as the representatives
of our Liassic forms in Bavaria.

A comparison of further genera and species from the Lias will show -
that we have representatives of nearly every form from Solenhofen
in our Lias beds.

EXPLANATION OF THE PLATES
(Illustrative of the genus Eryon).
Puate XXIV. figs. 2-4.

Fig. 2. Carapace of Eryon Brodiei, H. Woodw. Lower Lias, Lyme Regis. Two-
thirds the natural size. Collection of the British Museum.
3. Eryon Wilmcotensis, H. Woodw. Lower Lias, Wilmcote. Natural size.
Collection of R. F. Tomes, Hsq., F.Z.8.
4. Hryon Oppeli, H. Woodw. Lithographic stone, Solenhofen. Natural
size; from the original in the British Museum.

Pruatse XXV. figs. 1-3.

Fig. 1. Eryon Barrovensis, M‘Coy. Lower Lias, Barrow on Soar, Leicestershire.
One-half the natural size; restored from specimens in the collection
of the Rev. P. B. Brodie, M.A., F.G.S., and in the British Museum.

2. Eryon crassichelis, H. Woodw. Lower Lias, Lyme Regis. One-third
the natural size. Collection of Captain Hussey, Lyme.

3. Eryon Moore, H. Woodw. Upper White Lias, Ilminster. Twice the
natural size. Collection of Charles Moore, Esq., F.G.S., Bath. °

boc.

t Journ, Geol

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M&N.Hanhart care,

Sh URIAN “GRU LAwEAL,

1866. ] WOODWARD—DISCINOCARIS. 503

4. Ona New Genus of Puytiopopous Crustacea from the Morrat
Sues (Lianperto Fracs) Dumrrriessuire. By Henry Woopwarp,
Ksq., F.G.8., F.Z.S.

[PuaTe XXV. figs. 4-7.]

Havine lately received from Mr. D. J. Brown, of Edinburgh,
Specimens of shells, attributed to Discitna and Modiolopsis, from
Garple Burn, near Moffat, I examined them in conjunction with my
colleague, Mr. W. Carruthers, F.L.S.; and we were enabled, by the
help of these specimens and of others in Mr. Carruthers’s own collec-
tion, to determine them all to belong to one organism (folded in some
instances, and in others spread open), and that not a mollusk, but a
crustacean allied to Apus &c.

The fossil might readily be mistaken for the upper valve of a
Discina, haying a strong resemblance to Discina nitida from the
Carboniferous Limestone, and to Discina lamellosa, recent, from Peru ;
but upon a more careful examination nearly every specimen is
found to have in the front of the shell a wedge-shaped opening with
a well-defined border, which cuts the disk nearly to its centre*.

In a specimen from Mr. Carruthers’s collection (Pl. XXV. fig. 7)
the wedge-shaped sector which closes this opening remains in situ,
but the suture can still be detected.

In another specimen, from Mr. Brown’s collection (Pl. XXYV.
fig. 5), remains of the tail-segments are preserved on the same slab
with the folded shell.

The carapace, for such it must be considered, is ornamented by
concentric lines of growth, which curve slightly inwards upon reach-
ing the margin of the wedge-shaped suture in front. These con-
centric lines are finer and closer to each other near the apex, and
more stronly marked and further apart near its margin. The sector
displays similar concentric lines of growth with the rest of the cara-
pace. The form of the shell is slightly conical, as in Discina; but
many of the specimens, being crushed, do not show the normal form.
The apex of the shellis placed immediately behind the wedge-shaped
suture before mentioned.

In all the specimens yet seen no dorsal furrow can be detected,
the concentric lines passing smoothly in unbroken series around

“% Mr. Davidson, to whom Mr. Brown had submitted certain other more
‘minute shell-like impressions from these shales, thus writes concerning them
and the fossil at present under consideration :—

“33 Park Crescent, Brighton,
“97th October, 1865.

‘“‘ My pear Sir,—I send for your inspection the two specimens that were sent
to me by Mr. Brown, of Edinburgh, and which were derived from the Dum-
friesshire beds. They are certainly obscure fossils; but the specimens you
showed me were not Brachiopoda, but, as you said, remains of crustacea.

“Those I send show no indications of the fissure, or notch, and have a much
more Brachiopodous look than those in London. One of them somewhat resem-
blesa Lingula, the other a Discina; but I do not say they are Brachiopoda.

* * * * * * % * x * % *
“T remain, very truly yours,
(Signed) ‘‘THos. DAVIDSON.”

“ To H. Woodward, Esq.”

Oly XXIL,—PART I, 2M

504 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 23,

the posterior surface up to the margins of the suture. The absence
of a dorsal furrow at once separates it from Peltocaris Harknessi
and P. aptychoides (PI. XXY. fig. 6), allied forms of Phyllopodous
crustacea found in the same shales.

The wedge-shaped suture, which divides the shield of this crus-
tacean in front, doubtless corresponds with the suture in the shield
of Apus and the nuchal furrow in the Macrurous Decapods.

A similar line of separation has already been noticed in the shield
of Peltocaris aptychoides. (See Mr. Salter’s paper in the Quart.
Journ. Geol. Soc. vol. vii. pl. 21. fig. 10.)

Why, it may be asked, does the shield in this old crustacean, and
also in P. aptychoides, always separate along this line of suture, and
leave the appearance presented in the figure? (Pl. XXY. fig. 4.)

I can best explain this by referring to the recent Apus, in which
the footjaws, branchiz, and abdomen appear to be all strongly
united to the head, and that to the rostral portion of the carapace ;
whilst to the far larger posterior surface of the shield the attachment
is so slight that specimens always become detached in this manner,
and, as in the case of the phragmacone and sheath of the fossil Belem-
nite, the soft parts of the animal will often be found in one locality
and the carapaces minus the frontal portion in another.

Such is the case with Dithyrocaris, an allied genus, the organs of
manducation of which are seldom if ever found with the shields, but
in nodules (probably composed of the soft parts of the animal) i in a
bed by themselves*.

It may be interesting to record that among ae specimens from
Mr. Carruthers’s cabinet is a small example of Peltocaris aptychordes,
which exhibits the concentric lines of growth as in the Discina-like
form herein described. (See Plate XXYV. fig. 6.)

With the exception of Graptolites, fossils are of rare occurrence
in the Moffat shales. Mr. Salter has, as already stated, described+
two phyllopodous crustacea, Peltocaris Harkness: and P. “aptychoides,
Professor Harkness has found a small Brachiopod (Siphonotreta
micula, M‘Coy), and Mr. J. Stevens, formerly of Moffat, a single
specimen of Tentaculites.

The addition, therefore, of a new Phyllopod is an interesting dis-
covery. From its resemblance to Discina, I have proposed for it
the generic name of Discinocaris, and the specific appellation of
Browniana after Mr. D. J. Brown, who first drew my attention to it.

Dimensions.—Diameter of disk-shaped carapace 7 lines, sector
one-sixth of its arc. A larger specimen folded together probably
measured 14 lines in diameter.

EXPLANATION OF PLATE XXV. figs. 4-7.

(ilustrative of Discinocaris Browniana.)
Fig. 4. Discinocaris Browniana, H. Woodw. Moffat Shales (Lower Silurian), —
Dumfriesshire, Natural size. Collection of Mr. D. J. Brown,

* Geol. Mag. vol. ii. 1865, p. 401, pl. 11.
tT Quart. Journ. Geol. Soc. vol. xix. p. 87.

1866. ] PLANT—PRIMORDIAL FOSSILS. 505

Edinburgh. ‘The wedge-shaped rostral portion is absent from this,
specimen.

5. The same, in which the shield is folded together. Natural size. Col-
lection of Mr. D. J. Brown, Edinburgh.

6. Peltocaris aptychoides, Salter. Moffat Shales, Dumfriesshire. Three
times the natural size. Collection of W. Carruthers, Hsq., F.L.S.

7. Discinocaris Browniana, having the wedge-shaped rostral portion 7n situ.
Ae. size. Collection of W. Carruthers, Esq., F.L.S., of the British

useum.

5. Norrs relating to the Discovery of Primorprat Fossirs in the
Linevis-Fiaes i the Netaupournoop of Typpyn@w1LapiIs SILVER-
LEAD Mine. By Joun Prant, Esq., F.G.S.

[ Abstract. ]

Tx author recorded in this paper the discovery, during the autumn
of 1865, of fossils at Tyddyngwladis in beds belonging to the Lin-
gula-flags or Primordial zone, and partly referable to species known
to occur in other parts of Wales on the same horizon.

A detailed examination of the district, undertaken by the author
and Mr. E. Williamson, has enabled them to draw a section ex-
tending from the junction of the Lower and Upper Cambrians* at
Cefn Deuddwr to the base of Craig-y-Dinas, which was described
in detail} by the author.

The following list of the fossils found in the various divisions of
the Lingula-beds adopted by the author, and arranged in their order
of sequence, commencing with the lowest, have been prepared, after
Mr. Salter’s examination of the collection.

Tyddyngwladis Slates (Lower Lingula-beds). |

No. 1. Has not been examined. No. 2. Lingulella unguiculus, Salter.
No. 2, Anopolenus Henrici, Salzer. —, sp.
Salteri, Hicks, Obolella, sp.

, Sp. Protospongia fenestrata, Salter.
Paradoxides Hicksii, Sal¢er. {Dictyonema Graptolithinum?
Microdiscus punctatus, Salter. | No. 3. Agnostus, sp.

Agnostus Davidis, Salter. Obolella, larger sp.
princeps, Salzer. No, 4. Paradoxides Davidis, Salzer.

, Sp. Theca corrugata, Salter.
Theca, sp.

Cwm Eisen Slates (Lower Lingula-beds).

No. 5. Olenus cataractes, Salter. | No. 5. Agnostus trisectus, Sal¢er.
——, sp. nov. Track of a Trilobite.
Agnostus princeps, Salter. | Holocephalina, sp.

Hafod Owen Sandstones (Middle Lingula-beds).

No. 6. Olenus, sp. nov.. | No. 6. Hymenocaris ?

Conocoryphe, sp. nov. Annelid-tracks and. borings.
Lingulella Davisii, Salter. | +Buthotrephis (fucus).

* The Upper Cambrians of this author comprise the Lingula-flags, or base
of the Lower Silurian, of Sir Roderick Murchison and other geologists.
+ Published in full in the Transactions of the Manchester Geol. Soc. vol. v.
p. 220 e¢ seg.
_[ These are not Mr. Salter’s naming.

2u 2

506 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

Rhiwfely Slates (Upper Lingula-beds).
No. 7. Olenus (Peltura) scarabxoides, | No. 7. Spherophthalmus humilis, Phil.

Wahl. Agnostus princeps, Salter.
. Olenus spinulosus, Wahl. Lingulella lepis, Salter.
, Sp. nov., with longer Orthis lenticularis, Dalm.
spines. , Sp. nov.

| Moel Gron Slates (Upper Lingula-beds).
No. 8. Spherophthalmus _ pecten, No. 8. Olenus, sp. nov. with long head-

Salter. spines.
humilis, Phill. Agnostus princeps, Salter.

—— bisulcatus, Phil. trisectus, Salter.

alatus, Bech. , Sp. Noy.
Olenus (Peltura) scarabzoides, Conocoryphe Plantii, sp. n.,
Wahl. Salter.
tParabolina serrata, Salter. Conocoryphe, sp.

JUNE 6, 1866.

The following communications were read :—

1. On the Meramorpuic and Fossriirerovs Rocxs of the county of
Gatwa¥. By Professor R. Hanxnuss, F.R.S., F.G.S., Queen’s
College, Cork.

Txt portion of the county of Galway which lies between Killery Har-
bour on the north and Galway Bay on the south, includes Con-
nemara and Joyce’s country, one of the wildest and most moun-
tainous districts of Ireland.

A section of the geology of this district is given in Sir Richard
Griffith’s Geological Map of Ireland; and the rocks of the country
have been generally alluded to by Sir Roderick I. Murchison in the
last edition of ¢ Siluria.’

The rugged Connemara district is for the most part made up
of metamorphic rocks, among which patches of granite occur;
and this latter rock is found occupying a considerable area on the
south of the metamorphic series, and extending to the northern
boundary of Galway Bay. It also constitutes the rocky and moory
country known as Moycullen, which lies on the west side of Lough
Corrib. ,

The metamorphic rocks, as they are seen on the northern margin
of the granitic area, consist of gneissose strata, which strike east
and west, and which, although much contorted, have a prevailing
southerly dip, or incline towards the granitic area. On their northern
side rocks occurs a band of limestone, which can be traced west-
wards from a few miles west of Oughterard, on the shores of Lough
Corrib, for a considerable distance, as quarries of it are seen near the
road leading from Oughterard to Clifden. One of these appears near
where the Maame Road leaves the Clifden Road, at a spot called
Butler’s Lodge; and here the limestone is light grey in colour and
semicrystalline in structure. From Butler’s Lodge it passes west-

Section from Killery Harbour to Galway Bay (30 miles).

smog’
5 ATI
my TIS

Sas y

AY)
=N
NN

aA
Ges
Y,

SC eereweew =P)

HARKNESS—GALWAY.

d. Quartz-rocks. e. Granite.

c. Limestone.

4. Gneissose rocks.

a. Fossiliferous Silurians.

507

-wards through Shindilla Lake, and is

again seen on the Clifden Road at the
Halfway House, where it has a dip towards
the south at 45°. From the Halfway
House it is again seen at several spots,
where it has been worked, on the south
side of Clifden Road to near Recess.
About a mile north of Recess, at the
southern base of the hill called Lisoughter,
is a small village bearing the name of the
hill. Here the limestone again appears,
but considerably to the north of its former
line of strike, It exhibits at Lisoughter
its east and west strike, and passes under
eneissose rocks on its south side, but is
greatly contorted in its dips. At Li-
soughter it abounds in a dark-green
variety of serpentine (Loganite), and pre-
sents a darker colour than where it occurs
as amore easterly band. Besides abound-
ing in serpentine, the limestone at Li-
soughter also contains well-developed
radiated crystals of tremolite. A short
distance west of Lisoughter, at Coulma-
than, between Derryclare Lake and Lough
Inagh, it is again seen, and here has its
usual light-grey colour and its semi-
crystalline nature. A little to the south-
west of Coulmathan, on the margin of a
small bay on the eastern side of Derryclare
Lake, the limestone also occurs, having
serpentine imbedded in it, and exhibiting
the aspect which it presents at Lisough-
ter. From the eastern margin of Derry-
clare lake it extends westwards on the
northern side of the lake, and is again
seen on the southern side of Derryclare
Mountain. West of this it oceurs, in the
form of a dark-coloured serpentinous
limestone, in the lower course of a stream
called the Glencoughan River, which
flows from a wild deep gorge between two
of the Twelve Bens of Connemara, Bencorr
(2336 feet), and Benbreen (2276 feet).
The serpentinous limestone at Glen-
coughan River dips towards the south and
passes under the eneissose rocks. It has
on its northern side a mass of quartz-
rock, which is seen in the course of the
stream a short distance above the lime-

508 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

stone, and which dips south, or under the limestone. ‘The latter can
be traced, coming up in bosses or covered by a green band of vege-
tation, from the Glencoughan River, running parallel to, and a short
distance from, the Clifden Road, to a house called the Canal Stage,
where it crosses from the north to the south side of the road, whence
it still strikes westwards and passes beneath the waters of Ballyna-
hinch Lake.

The mass of limestone which les between the gneissose rocks and
the quartz-rocks probably exhibits itself, on the south side of the Con-
nemara Mountains, in more than one band. The limestone and its ©
associated strata have been greatly contorted in this part of the
county of Galway, and denudation has also aided in removing the
connecting links of the contortions—but not to such an extent as in
the country which lies on the north side of it; and by these agencies
the strata have been frequently repeated on the surface.

The quartz-rocks which occur on the northern margins of the
limestone give rise to the bold mountainous scenery of Connemara.
They form the Twelve Bens, and have in many spots a very
distinct stratification, and a strike which conforms with that of
the limestones. They are, among the Twelve Bens, thrown into
great anticlinals and synclinals; and in one of these latter, which
forms the east and west valley of the Owenglin River (the stream
which flows into the sea at Clifden), serpentinous limestone also
occurs. Between the Owenglin valley on the north and the lime-
stone band which passes under Ballynahinch Lake on the south,
there is an anticlinal of quartz-rocks. The upper portion of the
Owenglin valley is occupied by a district called Barnanoraun; and
here the principal quarries of serpentinous limestone occur.

The strike of these limestones here is also east and west; but the
dip cannot be made out, as the strata are excessively contorted.

The serpentinous limestones of Barnanoraun thin out towards the
east as they approach the quartz-rocks of Benbreen, the mountain at
the head of the valley. This thinning out, however, is the result of
denudation.

The north as well as the south margin of the valley of the Owen-
glin is flanked by quartz-rocks ; and the contortions which have taken
place among the rocks near the centre of the synclinal of the Owen-
glin valley have so far destroyed the original lamination of the
limestone strata as to open out irregular interspaces; and in some
cases the original limestone has disappeared, its place being supplied
by white carbonate of lime. The serpentinous limestone is here
much lighter in colour than that of the more southern band, owing
to the serpentine being of a lighter green colour than that which
occurs at Lisoughter and its neighbourhood.

With reference to the quartz-rocks of the Connemara district, the
arrangement of these and their relations to the limestones and gneis-
sose strata can be well seen in traversing the country which lies
between the Twelve Bens of Connemara on the west and the Maame
Tork range of mountains on the east. These ranges are separated
from each other by a wide valley having a north-west and south-

1866. ] HARKNESS—GALWAY. 509

east direction. In this valley is Lough Inagh, the only lake of a
considerable size in the Connemara country, which has a north-west
and south-east position.

The quartz-rocks are well exposed on the east side of Derryclare
Mountain and Bencorr.

They exhibit on this side of the range an anticlinal axis, on the
south side of which is the band of limestone before referred to; and
on the north side another band of limestone is seen in the valley of
Gleninagh. ‘This limestone of Gleninagh also occurs at Feliskin,
near the north-east side of Lough Inagh, on the road which is
now being made from the Clifden Road northwards to Kylemore.
As seen at Feliskin it is of a light-grey colour, and has the sub-
erystalline nature which the southern band exhibits where it is
not charged with serpentine. It dips from the anticlinal which lies
to the south of the limestone, and passes conformably under a small
area of gneissose rocks which occurs to the north of Feliskin.
The rocks, a short distance northwards, soon assume southerly
dips, the limestone here occupying a synclinal trough, which, if
followed over the mountains westward, would probably be found
to connect itself with the synclinal valley of the Owenglin River.
Some distance north of Feliskin another anticlinal axis occurs, on
the north side of which northern dips again prevail; and above the
quartz-rocks limestone again appears, succeeded conformably by
eneissose rocks, the latter being in their turn covered unconform-
ably by fossiliferous Silurian sandstones, which extend from near
Kylemore to the south side of Killery Harbour.

The valley in which Lough Inagh is situated so distinctly sepa-
rates the Maame Tork range of mountains from that of the Twelve
Bens of Connemara, as to justify the inference that it originated in
a fault. The Maame Tork range, on the east side of Lough Inagh,
presents very bold escarpments towards the south-west; and these
escarpments run very regularly north-west and south- east, the
direction which the assumed fault takes.

The arrangement of the metamorphic rocks of the west of the county
of Galway has an intimate relation to that which occurs among the
rocks of the same nature in the county of Donegal*. It also corre-
sponds with that of the Highlands of Scotland, representing the upper
“quartz-rocks, the upper limestones, and the upper or flaggy gneiss
of the latter country, as these have been described by Sir Roderick
I, Murchison.. With reference to the occurrence of serpentine in
connexion with the limestones of the metamorphic series of Con-
nemara, this has of late become a matter of some interest, in conse-
quence of the statement that these deposits afford the Hozoon Cana-
dense. The serpentinous limestones of Connemara are of local
occurrence ; they usually appear in such districts as exhibit the
strata highly contorted and broken up.

The lines of lamination in the limestone strata have been opened,
and the lamin have been fractured across, in consequence of the
contortions to which the strata have been subjected ; and into these
openings and fractures the serpentine has been subsequently intro-

* Quart, Journ. Geol. Soc. vol, xvii. p. 268.

510 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

duced. Serpentine doesnot, however, seem to have been the first
substance which occupied these cavities. The serpentine, on exposure
to atmospheric influence, frequently becomes much weathered, and
sometimes entirely disappears, leaving a crystalline skeleton in the
form of either tremolite, asbestos, or some other nearly allied mineral.
Asbestos is often found lining the sides of the limestone-cavyities in
decomposed specimens of serpentinous limestones on the east side of
Derryclare Lake. This mineral is here so arrangedas to present
the fine shell-structure alluded to by Dr. Carpenter as forming the
proper walls of the chambers of the Eozoon Canadense, and which
he speaks of as being “‘ made up of a multitude of extremely delicate
acicult standing side by side like the fibres of asbestos.”

Specimens of the serpentinous limestones from Lisoughter often ex-
hibit in some parts only the tremolitic skeleton, the serpentine proper
having disappeared. Specimens also occur in which portions of the
serpentine remain intact, while other portions gradually shade off
to the condition of tremolite.

The complex nature of serpentine has been frequently alluded to
by mineralogists, and also its varying composition. These cireum-
stances result from the variable amount and the variable nature of the
skeleton upon which the hydrous silicate of magnesia has been depo-
sited. In the case of the serpentinous limestone of Connemara, there is
good reason for inferring that the tremolitic and asbestose skeletons
were formed at the period when metamorphic action was changing
the purely sedimentary rocks. One of the most abundant minerals
produced by this metamorphic action was hornblende, a substance
which enters largely into the composition of the gneissose rocks
superposed on the limestones; and the tremolitic variety of this
mineral appears to have found its way into the cavities of the con-
torted limestones.

The following is the composition of tremolite from Fahlun :—

Sidi ert je fm sian cebraaeateniiad Nomae’siceavAama stasis aaa ater 60-10
WT aS AMC SIE TS. \eieiic le Aoninteateatsone sleet ose eiges ee eee 24:31
Tae aires wd od Spies alee he Sate te oe cee See eRe aera 12-73

Protoxide of iron variable.

tremolite being a silicate of magnesia and lime. The serpentine of
Ballynahinch has the following composition :—

SUITCA aia cars went yacetimimanis aR anc Ccen cae ES Slee Cece einer= eee 40:12 .
Magnesia ©. cccnr. sues cas eectes beau ues ad oaetneeseee eteeeaenes 40-04
A hamaiinal. 2° x. idaeia cetera eames ook Bee ee CUE cee ada eee 2:00
Protoxide 6faron® oleate Hees esa: eee eee ce eee 347
WAR. + isideia P25 Sotaiboraltse sate een Sedans vena eneeeh bee cee eee 13.36

98-99

The occurrence of serpentine in connexion with metamorphic
limestones is a common circumstance. It is found in association
with the limestones of Glen Tilt ; and here, as at Connemara, tremo-
lite is also. an accompanying mineral.

The supposed organic portions of the serpentinous limestones of
Connemara do not result. from animal structure, but purely from
mineral association. Had fossils of any kind presented themselves
in the limestones of this district, they ought to have occurred in

1866. | HARKNESS— GALWAY. 511

that portion of the limestone which has been least affected by meta-
morphic action. This is the character of the limestone which
occurs in that portion of the calcareous band which lies east of
Lisoughter, and which extends to near Oughterard. In this portion
of the band the lamine have not been opened and broken by con-
tortions ; and from it the serpentine is absent, and with this absence
of serpentine and its associated skeletons of tremolite and asbestos
everything like the so-called organic structure disappears.

The fossiliferous Silurian rocks of Connemara and of Joyce’s county
have been referred to by Mr. J. Kelly in a memoir “On the Grey-
wacké Rocks of Ireland’’*. They usually occur on the northern side
of the metamorphic range ; but there is one locality where this is
not the case—namely, on the western shore of Lough Corrib, at a
place called Shanballymore, about three miles north of Oughterard.
Here, to the north of a small patch of rather fine-grained granite,
and to the east of the metamorphic rocks, the fossiliferous Silurian
rocks are seen, consisting of a grey flaggy bed associated with thick-
bedded strata; but their relations to the rocks which margin them
are not seen here, and the fossils are principally procured from the
stones in the walls, which have been obtained from the loose frag-
ments scattered about the fields. Another fossiliferous Silurian
locality les at the northern end of Lough Corrib, a short distance
west of Cong. At the western extremity of this area the strata
come in contact with the metamorphic rocks of Benlevy (1375 feet),
and the relations of the fossiliferous beds to the rocks which margin
them are well seen. Here, at a short distance to the west of Lough
Coolin, which les under the eastern side of Benlevy, Silurian grits
occur nearly horizontal in position, but with a slight inclination
toward the N.N.E. Immediately west of these grits is one of the
bold escarpments of Benlevy, composed of gneissose rocks, which
strike east and west and are vertical in position.

Another locality from which we obtain information concerning the
relations of the metamorphic and the unaltered Silurian rocks is in
the valley which leads from Maame to Leenane, the latter being on
the south shore of Killery Harbour. In this valley there is astream
which flows from the north near Munterown, about three miles 8.E.
of Leenane. Where the road crosses this stream, at the bridge, a
conglomerate in the fossiliferous Silurian strata is seen; it abounds
in well-rounded fragments of gneiss and quartz-rocks, which have
been derived from the metamorphic series.

On the south side of Killery Harbour, at the head of a valley
called Glencraff, which runs from east to west, their relations are
also seen. The fossiliferous Silurian rocks form the hills on the
north side of the valley; they are well exposed, distinctly bedded,
and have an average dip towards the N.W. at 35°. The south side
of the valley consists of hills of gneissose rocks, with strata con-
torted, but having the usual east and west strike.

At Blackwater Bridge, on the road from Leenane to Clifden, and
about three miles from the head .of Glencraff, Silurian conglo-
merates are again seen, containing rounded metamorphic rocks ; and

* Journ, of the Geol. Soc. of Dublin, vol. viii.

4

512 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

immediately to the south-west of them the metamorphic strata
whence these conglomerates have been derived present themselves,
with the normal east and west strike.

The fossils which were collected by myself and by Mr. G. H.
Kinnahan, of the Irish Geological Survey, who accompanied me during
part of the time I spent among the fossiliferous Silurian strata of co.
Galway, are the following:—Favosites Gothlandica, Alveolites Labechii,
Halysites catenulatus, Petraia bina, P. ziczac, M‘Coy, Pleurodictyum
problematicum*, Phacops sublevis, M‘Coy, Encrinurus punctatus,
Fenestella prisca, Ptilodictya lanceolata, Atrypa hemispheerica, Orthis
reversa, Pentamerus oblongus, Spirifer plicatellus var. radians, Trochus
multitorquatus, Holopella obsoleta, Bellerophon.

The fossiliferous Silurian rocks of Galway, although on the whole
dipping from the metamorphic rocks on the north side of which they
repose, have many local irregularities. They are succeeded towards
the eastern end of Killery Harbour by grey- and purplish-coloured
pebbly grits, in which no fossils have yet been found.

These grits are false-bedded ; but their strike and dip seem to con-
form to those of the fossiliferous Silurian beds on which they repose.
They appear to form a synclinal trough near the head of Killery Har-
bour, as on the south side they have a northerly dip, and on the north
of this harbour they incline towards the south. These grits form a
very bold and rugged mountainous district, in which is Mweelrea
(2692 ft.), one of the highest mountains in this portion of Ireland,
at the northern entrance into Killery Harbour.

Eastwards from Killery Harbour these rocks appear in the form
of rugged precipices, forming the northern side of the mountains
which occur on the south side of the Errive River.

The grey and purple grits which overlie the fossiliferous Silurian
strata have a great lithological affinity to the so-called Old Red
Sandstones which occur to the south of the greenstones and fossili-
ferous Silurian (Caradoc) deposits of Pomeroy, co. Tyrone.

The fossils of the unaltered rocks of the west of Galway are such
as to indicate an horizon more nearly parallel with that of the Upper
Llandovery rocks than any other in the Silurian system. Of
these fossils, Atrypa hemispherica is by far the most abundant, and is
one of the most characteristic of the Upper Llandovery Brachiopods,
besides which we have a smooth Pentamerus. The Trilobite which
occurs most frequently is Encrinurus punctatus. With these fossils
other Upper Llandovery forms are found; and, although the corals
indicate a somewhat higher position among the Silurian rocks, the
whole facies of organic remains justifies the inference that the
fossiliferous Silurian strata of Galway belong to the middle portion
of the Silurian system.

* This, I have no doubt, is not strictly a fossil, but the cast of the upper por-
tion of the cup of a tabulate coral. On taking a cast of the Plewrodictywm above
mentioned, and comparing it with the upper surface of Favosites Gothlandica,
T could distinguish no difference in form. The tube-like body which so fre-
quently accompanies Plewrodictyum problematicum appears to be a cast of the
burrow of a parasite like the Sipunculus heterocyathus, which bored through
corals belonging to the genus Heterocyathus (vide Nat. Hist. Review, n. s., vol.

ii. p. 80).

1866. | J. GEIKIE—CARRICK, AYRSHIRE. 513

The metamorphic rocks upon which these beds repose have already
been referred to as the equivalents of the upper quartz-rocks, upper
limestones, and upper gneiss of the Highlands of Scotland. As the
position of these metamorphic rocks in the sedimentary series is now
known in consequence of the fossils which the Lower Limestone at
Durness has afforded, and as the position of this limestone is not lower
than the Llandeilo flags, we must refer the metamorphic action which
has changed the purely sedimentary rocks to an age later than the
Lower Silurian period.

Above the representatives of the Llandeilo flags there is, in the
Highlands of Scotland, a great thickness of quartz-rocks, lime-
stones, and gneissose strata; and the upper portion of this thick
series, in the form of the gneissose strata, very probably repre-
sents the Caradoc rocks. If this be the case, it follows that the
metamorphic action came into operation towards the close of the
Caradoc age. That the metamorphism of the gneissose rocks and
their associated strata was complete before the deposition of the
Upper Llandovery beds is proved by the occurrence, in the lower
portion of the fossiliferous Silurian rocks of Galway, of conglomerates
full of metamorphic fragments. All the circumstances which bear
evidence as to the period when metamorphism took place among the
altered rocks of this part of Ireland place this period in the Lower
Llandovery epoch. If this inference be correct, it must be extended
beyond the western portion of the county of Galway ; for it will em-
brace not only the whole of the metamorphic rocks of Ireland, but
also all those of the Highlands of Scotland, except the Funda-
mental or Laurentian gneiss.

2. On the Meramorpurc Lower Sinvurran Rocxs of Carricr, AYR-
soire. By James Gerxie, Esq., of the Geological Survey of Great
Britain.

(Communicated by Professor A. C. Ramsay, LL.D., F.R.S., V.P.G.S.)

ConTENTS.
I. Introduction. B. Felspar-porphyry.
II. Felspathic rocks. Recapitulation and statement of
A. Amygdaloid. inferences.
Succession of changes :— C. Brecciiform rocks.
1a. Unaltered strata. D. Finely crystalline felstones.

16. Slightly altered strata: ori- | III. Dioritic rocks,
ginal character quite apparent; | IV. Serpentine.

bedding distinct. 1. Schistose serpentine.

2. Granular strata with spora- 2. Compact serpentine.
dic vesicular and amygdaloidal 3. Association of diorite and ser-
areas: bedding distinct. pentine.

3. Amorphous green paste-rock | V. Limestone.
with pseudo-bombs: bedding Association of serpentine with
lost. calcareous strata.

4, Felspathic amygdaloid. VI. Conclusion.

I, Inrropvcrion.
Tue metamorphic region which forms the subject of this commu-

514 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

nication was traversed by Sir Roderick Murchison, accompanied by
Professor J. Nicol, in 1850; and the former geologist subsequently
published the results of that journey, in a memoir upon the geology
of the South-western Highlands of Scotland*; but as the end Sir
Roderick had in view was mainly to ascertain the structure of the
strata and determine their position, his allusions to the metamorphic
rocks are necessarily brief. In the spring of 1865 the Geological
Survey was extended into the southern regions of Ayrshire, and thus
afforded my colleagues (Dr. Young and Mr. A. Geikie) and myself
ample facilities for a more minute examination of the beds in ques-
tion. We recognized the metamorphic character of certain diorites,
serpentines, and crystalline felspathic rocks, independently of each
other ; and in the area that fell to me to survey I was enabled to
trace passages between the various altered rocks, which seem to
throw light upon the obscure process of metamorphic action. The
interest which is attached to the altered strata of this district chiefly
consists in the fact that they exhibit certain arrested stages of
metamorphic action, so that we can in many instances begin with
unaltered beds and trace the gradual changes which they undergo
during their passage into crystalline and pseudo-igneous rocks. The
large masses of amygdaloid indicated upon the sketch map which
accompanies Sir Roderick’s memoir, notwithstanding their exceed- .
ingly igneous aspect, are nevertheless, as will be shown, not of
igneous but of metamorphic origin. Of the same nature are the
porphyries, diorites, and serpentines. The resemblance to trap
which many of those rocks exhibit is so striking that it will per-
haps be difficult to convince a geologist who has not minutely
examined the ground for himself of their true character.

With Sir Roderick Murchison’s permission, some of the more
interesting results obtained during the progress of the Survey are
here described.

The metamorphic Lower Silurian rocks surveyed by us may
be roughly estimated to cover an area of forty-five square miles
or thereabouts. They extend in the direction of the strike (2. e.
N.E. and 8.W.) for ten miles or so, with an average breadth
of three miles and a half; but several isolated portions occur
beyond the main mass of metamorphic strata. Beginning a
little to the south of Girvan, the altered rocks continue, with
little interruption, along the coast-line as far as Currarie Port
—a distance of about twelve miles. As the coast-line cuts the
strata at an acute angle to their strike, nearly all the varieties of
metamorphism characteristic of the district are met with in this
section. The northern limits of the metamorphic area are exceed-
ingly irregular. ‘The lines traced by us in that direction show altered
beds extended among unaltered deposits ; and the boundary is still
further confused by faultings, and by overlaps of Old Red Sand-
stone. Towards the south, however, the metamorphic strata are
separated from the unaltered greywackés by a long wavy fault which
runs inland from the sea-coast at Glendrishaig, and, keeping to the

* Quart. Journ. Geol. Soc., vol. vi. p. 137 bis.

1866. ] J. GEIKIE—CARRICK, AYRSHIRE. 515

line of strike (S.W. to N.E.), terminates at Pinmore Bridge on the
river Stinchar, where it is cut off by another fault coming from
the west.

The metamorphic rocks usually dip at a high angle, while the
strike corresponds in a remarkable degree with that of the unaltered
strata of the surrounding country. On the Survey-maps we have
distinguished three great groups of rocks, viz. Lelstones, Diorites,
Serpentines.

Felspathic rocks are by far the most abundant, and are very
varied in structure and aspect. The diorites and serpentines, on
the other hand, have a more definite character, and are usually
interbedded or very closely associated. It is worth noting, that, if
we traverse the strata from south to north, we shall find that inter-
bedded diorites and serpentines alternate with great belts of felspa-
thic rock. Thus, starting from the fault which forms the southern
boundary of the metamorphic rocks, we first cross amygdaloidal,
finely crystalline, and brecciiform felspathic rocks. Thereafter, as at
Balhamie Hill, we come upon serpentine with associated diorites.
Leaving Balhamie Hill, we again pass over a belt of felspathic rocks,
until, at Carleton Hill and Lendalfoot, we find ourselves once more
among diorites and serpentines, and so on with the beds to the north.

The bounding fault on the south unfortunately throws some doubt

on the relation which the metamorphic rocks bear to the unaltered
strata. But, notwithstanding the south-east dip of the latter, the
downthrow is to the north; and therefore the metamorphic strata
must occupy a somewhat higher horizon than the unaltered wackés
against which they abut. Little isolated portions of metamorphosed
rock are met with here and there among the unaltered greywackés
alluded to, often far removed from the chief area of metamorphic
strata; but an account of their probable origin and connexion with
strata denuded away is reserved for a forthcoming memoir of the
Geological Survey. Several areas of unaltered strata, enclosed and
surrounded on all sides by metamorphic rocks, will be described
below as representing the nature of the beds which have become
metamorphosed. The unaltered strata of this region exhibit the
usual character of the Lower Silurian greywackés and shales of the
southern uplands of Scotland. They are all strongly felspathic,
but are usually more highly impregnated with alkaline matter than
the Silurian rocks of Berwickshire, Peeblesshire, Selkirkshire, and
other districts which have been examined by the Survey. Many
of the beds effervesce freely with acids, showing the presence
of lime, while the abundance of magnesian matter has often tinged
the rocks with green. Immediately south of the metamorphic region,
the unaltered Silurian strata are not markedly magnesian, but they
still contain in places a not inconsiderable admixture of calcareous
matter.
- At present attention is directed to a generalized description of
the metamorphic strata, for the purpose of tracing the various
stages in the process of alteration, and of thereby attaining to some
knowledge of the causes which haye induced metamorphism,

516 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

The strata to be described consist of felspathic rocks, diorites,
serpentines, and altered limestone and calcareous greywacke.

Il. Fetspataic Rocks.

The felspathic rocks cover a large area in the metamorphic region
under review. They are exceedingly well exposed along the sea-
coast, where they rise into rugged broken cliffs, fissured with num-
berless inlets and retiring coves. Very good sections are also
obtained in the streams that drain into the Stinchar, while the hill-
sides themselves are roughened with fine exposures of the same
rocks. These felspathic masses consist chiefly of four varieties—
amygdaloid, felspar-porphyry, brecciiform rocks, and finely ecrystal-
line and compact felstone,—all of which are closely related, both
as regards the manner of their occurrence and the mode of their
formation.

. A. Amygdaloid.

The felspathic amygdaloids are largely developed throughout the
district, but may be best studied along shore, between Knockgowan
Hill and the mouth of the river Stinchar, and at many points on the
coast-line north of Bennane Head. ‘They are also very well seen at
numerous places along the line of fault that separates the meta-
morphic rocks on the north from the unaltered greywackés to the
south. They have, in general, an exceedingly igneous aspect,
especially on the coast, where they form rugged stacks, and weather
into rough lumpy-shaped masses on the cliffs. Seen from above,
the igneous character of these rocks could scarcely be doubted.
Where they are most typically developed, they often look as if made
up of large bombs—an appearance which not infrequently gives place
to a columnar structure. A closer inspection shows us their
abundant amygdaloidal cavities; and these, taken in connexion with
the roughened and sometimes almost trachytic surface of the stone,
seem at first sight to indicate a former state of igneous fusion.

Colour, Composition, Texture, Fracture.—The prevailing colour of ©
the amygdaloids south of the Stinchar is a pale greyish blue, passing
into dark green and grey; north of Bennane Head they generally
assume a light purplish brown, with occasional areas of greyish blue.
The matrix consists of a paste of felspathic matter, with here and
there a variable admixture of magnesia and lime. In texture these
amygdaloids sometimes resemble the felspathic traps of the Ochils,
the Pentlands, and other Old Red regions. This, especially, is the
case with those light-purplish-brown varieties which lie exposed
along the shore to the north of Bennane Head. The harder portions
of the rock show a very finely crystalline texture ; but in the more
alkaline and earthy areas crystals can seldom be detected, the
matrix appearing like a fine felspathic mud, shot here and there
with a few minute points of felspar. In the district south of the
Stinchar, the felspathic amygdaloids seldom exhibit this earthy
texture ; on the contrary, the matrix is harder, less alkaline, and
more generally crystalline, but always very finely so. The fracture

1866. ] J. GHIKIE—CARRICK, AYRSHIRE. 517

varies, of course, with the texture of the rock; it is usually rough
and irregular, like that of many traps, but sometimes conchoidal.

Amygdaloidal Cavities. —The amygdaloidal cavities are very
abundant, but are often partially aggregated in areas, leaving the
surrounding portions of the matrix less profusely pitted. They
invariably assume a globular shape, except where two or more have
become confluent, when the cavity resulting from their union is
usually of irregular form. They are of all sizes, from mere points
up to globules as large asa sweet pea; but larger cavities are not un-
common. Perhaps the most abundant sizes are those which may be
compared to turnip and mustard seeds. Carbonate of lime is the
mineral most usually met with in these cavities; but zeolites and
decomposing magnesian minerals are abundant in places; hard
white felspar is also occasionally met with.

The most continuous exposure of the rocks in question occurs
along the coast, between Knockgowan Hill and the river Stinchar.
Throughout this section the bedding is often very distinct, the
strike corresponding with that of the unaltered greywackés of the
adjoining districts, viz. N.H. and S$.W. But frequently all trace of
bedding is lost, even when the rock-masses are viewed from a little
distance. Here and there occur bands of a hard and highly altered
red greywacké mudstone passing into Lydian stone ; and occasionally
we come upon portions of fine pebbly and brecciated greywacké,
resembling at a first glance the comminuted paste of a volcanic ash.
Courses of greywackeé, distinctly granular, alternating with thinner
bands and shales, also make their appearance in some parts of the
section. All these regularly bedded and undoubtedly aqueous rocks
are interstratified with, and, when their strike is prolonged, seem to
pass into, felspathic amygdaloid and finely crystalline felstone.

It has been stated that a first view of the amygdaloid would lead
one to infer an igneous origin for that rock; to one, however, who
had previously explored the greywackés of the surrounding country,
and familiarized himself with their texture and mode of weathering,
this apparently igneous aspect is not always so strikimg. In many
places the greywackés of the non-metamorphic regions are exceed-
ingly hard, and sometimes approach to crystalline in texture. More-
over the weathered crust of the amygdaloid, like that of the grey-
wackés, is seldom more than a line or so in thickness ; and the rock
when broken shows a very general absence of that dull earthy tex-
ture which among Scottish traps usually attends an amygdaloidal
structure.

From the distinctly bedded nature of the amygdaloids, and their
alternation with other rocks to be described in the sequel, these
masses, if of igneous origin, are manifestly not intrusive. On the
other hand, if we believe them to have been poured out at the earth’s
surface, we shall look in vain for those flattened amygdaloidal or
vesicular cavities so characteristic of true amygdaloidal trap. The
shape of the vesicles, as already mentioned, is invariably spherical.
If this appearance were confined to certain limited areas, or only
showed itself irregularly here and there, we could not consider it

518 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

anomalous; but when we meet with the same spherical cavities
throughout the entire mass of the amygdaloidal beds over an area
many square miles in extent, it seems difficult to believe that the
beds in question could ever have been in motion like any ordinary
streams of molten rock. These and other considerations threw
doubt upon the apparently igneous character of the rocks under
review; and a careful examination of the district north of the
village of Ballantrae eventually revealed their truly metamorphic
origin. ‘The coast-section north of Bennane Head first yielded what
are considered to be the proofs of this metamorphic action. The
same appearances frequently recurred in other places; but a con-
densed description of the part of the coast-section alluded to will
perhaps suffice for the present.

Between Balcreuchan Port and Port Vad a most interesting series
of rocks is laid bare. Distinctly bedded greywackés and shales
occur sporadically, but are quickly surrounded on all sides by con-
fused felspathic masses, for many of which we should require special
names. Felspar-porphyries, felstones, amygdaloids, a remarkable
green rock stuck full of stones, and brecciiform masses which look
as if they had been violently pounded up in place are some of the
varieties we meet with.

Succession of Changes:—1 a. Unaltered Strata——The most un-
altered beds hereabouts are red, brown, and greyish sandy greywackés.
In places they are particoloured, showing yellow and green blotches,
owing to the decomposition of alkaline matter, with which all the beds
appear to be more or less charged.

1 b. Slightly altered Strata—The next beds to be noted are
more hardened, and often have a baked appearance; they also con-
sist of ereywackés—green, brown, red, and purplish blue. The dirty-
green beds are always highly magnesian and calcareous; the grey
and brown beds less so; the red beds still less so, often apparently
with no recognizable amount of alkaline matter. The same may be
said generally of the purplish-blue varieties, which, however, are
not of common occurrence along this part of the coast. All these
beds are much jointed, often to such an extent that they crumble
down into little angular fragments. This is markedly the case
with the compact red shales. The stratification is frequently contorted
and crumpled.

2. Granular Strata with Vesicular Areas.—A little south of Bal-
creuchan Burn the greywackés upon the shore exhibit some very re-
markable appearances. These beds, although altered to some extent,
still show well-marked bedding, and are in places quite granular.
Little specks of a reddish-brown shale, similar to the small hardened
clay-galls in the greywackés of Peeblesshire, were occasionally de-
tected. The beds are felspathic, and have a greenish tinge from the
abundance of magnesian matter which they contain. Carbonate of
lime also enters somewhat largely into their composition. Completely
isolated and surrounded on all sides by this comparatively unaltered
ereywacké occur several vesicular areas. The matrix of these areas
has the same general character as the rest of the beds, ce in

1866. ] J. GEIKIE—CARRICK, AYRSHIRE. 519

this only, that it never is pebbly or granular. They vary in diameter
from a few inches to a foot and upwards across. In the smaller
areas the form assumed is irregular ; but as they increase in size they
become bomb-shaped or rudely spherical. The amygdaloidal vesicles
are always round, save where two or more have coalesced to form
a confluent ragged cavity. They vary in size from that of the finest
seed up to vesicles with kernels hike small sweet peas. Larger
cavities than this are rare. The ‘“‘sweet-pea” cavities are for the
most part aggregated towards the centre of a vesicular area, the
vesicles decreasing in size as they approach its circumference. In
this way each little amygdaloidal area shades off imperceptibly into
the unaltered greywacké in which it appears to be imbedded. Outside
of such an area the greywacké has usually a pasty aspect, not unlike
the dull matrix of some highly basic trap, but not infrequently a
granular texture; and even small specks of dark shale may be
obtained only a few inches from the amygdaloidal portions of the
rock. The vesicular areas most commonly occur not far from each
other, but often they lie widely apart. We may obtain them in
contact, or from an inch to several yards asunder, the intervening
parts of the bed being always destitute of amygdaloidal structure,
and frequently showing a granular and sometimes even pebbly tex-
ture.

The rocks which have just been described exhibit well-marked
bedding, and alternate in places with coarse shales. The softer
beds weather away, leaving the harder bands isolated; the joints
are like those of typical greywacké, square, sharp, and well defined.
In short, the general appearance of the beds is quite that of the
Lower Silurian rocks in the unaltered regions of the surrounding
country.

3. Amorphous Green Paste-rock.—In the peculiar masses that
have next to be considered all trace of bedding has disappeared ; the
jointing is obscure and ramifying, and the general aspect of the
rocks as unlike any regularly stratified deposit as it could well be.
The masses referred to consist of a greenish pasty matrix, thickly set
with felspathic bombs. At first sight the rock closely resembles a
volcanic ash, and, as seen from the cliffs above, one would scarcely
hesitate to callit so. The tough felspathic matrix weathers away
with a rough, almost trachytic surface, leaving the bomb-like stones
standing outin relief. It most usually assumes a dirty greenish hue,
sometimes a dark brown. The texture is dull, like that of those por-
tions of greywacké already described as encircling a vesicular area.
We may define the matrix shortly as a greenish alkaline felspathic
paste in which no distinct crystals are apparent. The pseudo-
bombs are of all sizes, from fragments only an inch or two across to
blocks several feet in diameter. When broken, their weathered
crust is found to be only a line or so in thickness. They consist of
purplish-blue and brownish-red felstone, fine-grained, and look as
if they might all have been derived from one bed of felstone. The
usual globular amygdaloidal cavities are also characteristic of nearly
all the pseudo-bombs. These pseudo-bombs are therefore considered

VOL, XXII.—PART I. 2N

520 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

to be identical in origin with the vesicular areas of the less altered.
greywacké beds. They occur in greater abundance than these last,
thus eyincing a more advanced stage of metamorphism—an inference
which is further strengthened by the pasty aspect of the green
felspathic matrix. The larger pseudo-bombs generally approach to.
a rounded form, and increase in numbers until they often impinge,
and by their union form spheroidal masses of felspathic amygdaloid.
When the pseudo-bombs press closely, the structure of the rock be-
comes columnar. The passage into felspathic amygdaloid can thus
be distinctly traced.

4, Felspathie Amygdaloid.—A general description of the amyg-
daloid has been given above; but a few additional notes may be
added here. It shows most usually a spheroidal structure; when
it becomes columnar, the columns are found to obey no order in the
mode of their occurrence. They seldom continue long in one direc-.
tion, but occur at all angles to any given plane. Between this rock
and the green paste-rock (or nascent amygdaloid) there is, as just
pointed out, a close relationship. We therefore find the two rocks,
intermingled and blended in a very confused manner. Taking a,
general view of this part of the coast, however, there appears to be
a rude alternation of pseudo-ashy beds with felspathic amygdaloid..
Examined in detail, no such arrangement is visible. Here may be
seen an irregular area of pseudo-bombs projecting from their green
paste, surrounded on all sides by felspathic amygdaloid; there,
again, may appear amorphous masses of amygdaloid completely
enclosed in “ green paste-rock.” The amygdaloid becomes in places.
porphyritic with felspar, and passes into felspar-porphyry. During
this passage the matrix gradually loses its basic appearance, and
the amygdaloidal cavities decrease both in numbers and size. The
rock thus insensibly shades into felspar-porphyry.

B. Felspar-porphyry.

This is an intensely igneous-like rock. The felspathic matrix,
which is sometimes sparingly magnesian, is of chocolate-brown
_and red colour, with a dull hard compact texture. It is pro~
fusely porphyritic, with tabular crystals of greyish felspar. Some-
times little spherical cavities may be detected in the body of
the rock; but this is rare. At its junction with comparatively
unaltered greywacké, however, the felstone is in some places punc-
tured with numerous vesicles, which vary in size from mere pin-
points up to the usual small “ sweet-pea” cavities. In its central
portions the rock is amorphous, but at its junction with greywacké
it sometimes shows a spheroidal structure. The phenomena exhi-
bited both by the felspar-porphyry and the greywacké on these
occasions deserve attention. At the foot of Balcreuchan Burn we
come upon an area of well-bedded greywackés, completely sur-
rounded on all sides by crystalline rocks. The greywackés are
often much crumpled and infinitely jointed, and some portions haye
undergone a peculiar brecciating process which will be described in
the sequel. On their upturned ends rests an irregular cap of fel

1866.] J. GEIKIE—CARRIOK, AYRSHIRE. 521

spar-porphyry, which here assumes the character of an overlying
trap, with a most uneven bottom. At its southern boundary it
presents some remarkable appearances, losing its usual amorphous
nature and becoming largely spheroidal. The spheroids have a
reddish hard-glazed exterior, and show innumerable spherical cavi-
ties like mere pin-punctures, but occasionally larger.. The spheroidal
masses measure from two or three to five or six feet in diameter. At
their junction with the greywacké, the portions visible are encased
in shells about half an inch in thickness of hard fine-grained
reddish greywacké, much jointed, and sometimes crystalline like
felstone. ‘To what extent the porphyry spheroids are enclosed in
these peculiar greywacké shells or cases was not ascertained. When
two spheroids impinge, the “case” in which each is enveloped
appears as if it had been sucked in between the rounded masses
of felspar-porphyry. The shells may be separated from the rock ;
and their inner surfaces are then found to be coated with porphy-
ritic felspar crystals; but these crystals nowhere penetrate beyond
the surface, to which they appear to be merely adherent.

In other places, where enveloping shells or cases are wanting, a
distinct passage can he traced from the porphyry into the greywacké.
The porphyritic crystals become gradually smaller, until at last they
disappear, and thus leave a red compact or finely crystalline fel-
stone. ‘This rock, again, shades off into hard reddish greywacke.

The passage from amygdaloid into felspar-porphyry has been
given above; the latter, indeed, is most commonly associated with
the former.

Recapitulation.— Before attempting to describe the other forms of
metamorphism displayed in this district, I may recapitulate some of
the facts advanced, and state the inferences which seem to be fairly
deducible from them.

An examination of the less altered rocks of the metamorphic
region will show that the strata are of variable composition, some
portions being more highly alkaline than others. The large amount
of calcareous, and especially of magnesian matter is indeed very
striking. This alkaline character of the strata may be considered
one of the causes of that intense metamorphism to which many of
the beds have been subjected; for those which contain the largest
admixture of alkaline matter appear to have been peculiarly sus-
ceptible of change. The green magnesian and calcareous grey wackés
are often studded with vesicular and. amygdaloidal areas; on the
other hand the less alkaline deposits are frequently merely har-
dened, without assuming any pseudo-igneous structure. A broad
general view of the whole series of strata thus gives alternating masses
of more or less distinctly crystalline and altered rocks; but when
viewed in detail the various metamorphic rocks are generally found
to be confusedly mingled together, interlacing and blending in the
most irregular manner. |

The little patches of unaltered greywacké which occur here and
there in midst of metamorphic strata are interesting, ay they seem

to throw some light upon the process by which the felstones, amyg-
2n2

522 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

daloids, and porphyries have been produced. Regarding the origin
of the isolated amygdailoidal areas two opinions may be held. We
may suppose the cavities to have been formed by gases during a
pasty condition of the rocks, and the amygdaloidal minerals to have
been subsequently introduced. In this case the origin of the vesicles
would be entirely analogous to that of the cavities in lava. But
evidence is not wanting which seems to lead to the inference that
the vesicular nature of the altered wackés may be due to segregation,
the excess of alkaline matter having separated from the felspathic
matrix to store itself up in little globules. [The same kind of
phenomena may be seen in many trap-rocks. Globules of quartz,
which are clearly not due to infiltration, abound in some felstones,
and they have also been detected in other igneous rocks.]| Towards
the centre of an amygdaloidal area the vesicles are largest, and from
the centre outwards they gradually decrease in size, until they be-
come so small as to require a lens to distinguish them. In this
manner amygdaloidal areas shade off into the unaltered granular
portions of a wacké. It would seem, therefore, that, as long as the
metamorphic action procecded, the vesicles increased in size until
they had reached their maximum*. Towards the circumference of
an area, as the action extended, the vesicles, it may be supposed,
continued to expand by receiving fresh supphes of gaseous matter.
The metamorphism, however, having suddenly ceased, left its work
incomplete; and thus we find the smallest cavities at the edge, and
the larger ones in the centre, of an amygdaloidal area. That vesicles,
however, may have been formed by the segregation of amyg-
daloidal mineralsf is rendered probable by the fact that the matrix
in which they occur is commonly harder and more compact (in
other words less alkaline) and of a darker colour than the sur-
rounding wacké. It has also been pointed out that the hard
non-alkaline beds with which the softer magnesio-caleareous
wackés are interstratified have remained comparatively unaltered.
So far as was seen they are never amygdaloidal. The num-
ber of globular cavities is always greatest where the rock
undergoing alteration is most highly alkaline. Of course, it must
be admitted that these appearances are also explicable on the
assumption of the gaseous formation of the cavities; for the same
action which could only impart a crystalline or semicrystalline
texture to less basic strata might reduce highly alkaline wackeés to
a pasty condition in which gas-cavities would readily form. But,
although the cellular character of these metamorphic rocks is doubt-
less mainly due to the expansive power of imprisoned gas, yet the
occasional origin of the cavities by segregation must not be overlooked.
Future chemical analyses will enable us to clear up this point.

* When the cavities are very closely aggregated, they are usually smaller
than when they occur in less numbers. re

t I refer here to cavities of magnesian and calcareous matter; it has been
already stated that, associated with these minerals, zeolites and hard white felspar
also occur in some places. Whether (on the supposition that the cellular nature

of the rock is due to segregation) the zeolites and felspar are contemporaneous
with or have supplanted the alkaline minerals can only be conjectured.

1866. ] J. GEIKIE—CARRICK, AYRSHIRE. 023

The amorphous green paste-rock with its pseudo-bombs, it was
said, is only a more altered greywacké, the pseudo-bombs corre-
sponding to the amygdaloidal areas of the distinctly bedded and less
altered wackés. The whole appearance of this peculiar rock be-
tokens a greater degree of metamorphism. _ The bedding has gone;
the amygdaloidal areas or pseudo-bombs are in greater abundance ;
and their matrix is harder, and sometimes even semicrystalline.
The manner in which these pseudo-bombs become aggregated,
so as to form by their union masses of felspathic amygdaloid, has
been described above. : :

It may be objected to this that the green paste-rock, instead of
exhibiting an arrested stage of metamorphism, may be merely the
decomposing wacké of an igneous rock. But the pseudo-bombs do
not exfoliate like the spheroidal portions of a decomposing trap ;
their weathered crust (seldom thicker than a penny) is itself quite
hard. The composition of the green paste differs considerably from
that of the pseudo-bombs: the latter show apparently no alkaline
matter, save in their amygdaloidal cavities; while the former is
abundantly charged with it, and in its unweathered portions it has
the same composition. It is difficult to believe that a rock so con-
stituted could have resulted from the decomposition of a felspathic
trap. If the pseudo-bombs were the only solid parts remaining of
such a decomposed and weathered trap, we should expect to find
them shading off into the surrounding decayed portions of the bed.
But nothing of this is apparent. Their junction with the green
paste is so sharply defined, that no one who sees that rock can for a
moment suppose it to have resulted from the decomposition of a
felspathic amygdaloid having the same mineralogical character as
the pseudo-bombs. Bearing in mind the occurrence of distinct
amyegdaloidal areas in well-bedded and granular greywacke, I am
convinced that in the green paste-rock we have just the same
phenomena, but in a higher state of development.

_ The felspar-porphyry must be regarded as the maximum stage of
metamorphism exhibited by the felspathic rocks of the district. The
passage from granular sedimentary beds into this very igneous-like
rock can be so well traced as to leave no doubt of its metamorphic
origin; while the peculiar junction of its spheroidal portions with
comparatively unaltered greywacké is quite unlike any junction of
igneous and aqueous rocks. he manner in which the shells or
cases are moulded round the spheroids of porphyry appears to indi-
cate that they were once in a sufficiently pasty condition to allow of
their being pressed outwards by the increasing spheroids of felstone.
But it would almost seem as if their want of alkaline matter, by
rendering them less easily assailable, had stopped the further pro-
gress of the metamorphic action in their direction. It is certainly
_yery remarkable that, although we find the felspar crystals of the
porphyry well developed on the surfaces of the spheroids, and even
coating the concave side of the shell-cases, we yet cannot detect
here a passage from the one rock into the other. Upon the whole,
it is perhaps preferable to regard the cases of hard reddish rock as

524 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

merely a stage in the metamorphism. We may suppose the por-
phyry spheroids, during the period of their outgrowth, to have been
constantly surrounded with a paste of felspathic matter, in which
the felspar crystals were generated. Thus, as the metamorphism
proceeded, case after case would become obliterated and absorbed
into the body of the rock, while, at the same time, new cases of
felspathic stuff would continue to form on the fresh surface of each
outgrowing spheroid.

The felspar-porphyry is only very sparingly amygdaloidal. The
surface of the spheroidal portions is, indeed, often abundantly pitted ;
but the body of the rock rarely if ever shows any amygdaloidal
cavities ; nevertheless a passage from amygdaloid into felspar-por-
phyry may occasionally be traced. Some greywackés must there-
fore have passed through the stages of “ green paste-rock” and
amygdaloid before they at last became metamorphosed into felspar-
porphyry. But the gradation to be observed from granular grey-
wacké into finely crystalline felstone, and from that into porphyritic
felstone, shows us that porphyry may sometimes be produced directly
from aqueous rocks without an intermediate vesicular stage. All will
depend upon the composition of the rocks undergoing alteration.
If they are highly basic, a vesicular condition will probably precede
the production of porphyry; if, on the other hand, the beds are
less basic, a previous vesicular stage does not seem necessary to the
formation of porphyritic felstone.

C. Breeciiform Rocks.

The anomalous brecciiform beds which are now to be described
are of sporadic occurrence. Followed along the general strike of
the strata they quickly die out, even when they have attained a
considerable thickness. They are typically developed on the coast
near Bennane Head, and the beautiful hill of Knockdolian is made
up of them. No description ¢an convey an adequate notion of their
character. Knockdolian Hill consists of a mass of brecciiform rock,
entirely amorphous and unstratified, except in one or two places,
where, however, the appearance of bedding may be due to jointing.
The brecciiform fragments are of all sizes, from mere dust up to
stones twice the size of a walnut; but much larger fragments are
common enough: while most are of angular shapes, many haye a
somewhat rounded and subangular aspect, often bearing a striking
resemblance to the small lapilli of a volcanic ash. They consist of
fine-grained and compact felspathic rocks. Matrix is usually want-
ing, but is sometimes present in meagre quantity: when it occurs
abundantly, the rock has all- the appearance of a scoriaceous ash ;
and on such occasions it sometimes becomes difficult to distineuish
it from the green paste-rock. The composition of the matrix is
chiefly felspathic, with an admixture of crystalline carbonate of lime
in some places. But, as just remarked, matrix is for the most part
wanting, and the stones are huddled together in the direst con-
fusion. In the rock of Knockdolian Hill one or two rounded stones
were obtained, whose smoothed surfaces told their story of former

1866. | _ ‘J, GEIKIE—-CARRIOK, AYRSHIRE. 525

attrition by water. But how they had come to be imbedded in the
angular breccia, and what the origin of that breccia could be, there
was no evidence in the hill to show. An examination of the coast-
section, however, was more successful. Near Bennane Head the
high road skirting the sea overlooks a large mass of Knockdolian
rock. The shape of the stones hereabouts generally approaches to
roundness, but they are often of very irregular form. Water-worn
stones, some of them six inches across, are here not uncommonly
intermingled with the angular and subangular fragments of which
the great bulk of the rock consists. Some of these rounded stones
show only a partially water-worn surface, the other portions being
roughened and subangular. Such water-worn stones increase in
number until we find them, in one place, forming a rude band, the
direction of which corresponds with the strike of a little area of
unaltered stratified wacké, which is here completely surrounded by
amorphous Knockdolian-rock. It is noteworthy that the smoothest
and more perfectly rounded stones are those composed of the hardest
and most compact rock; while those which have lost their smoothed
surfaces consist of less hard and compact rock and are very gene-
rally amygdaloidal, the vesicles being of the usual spherical shape.
We are therefore justified in concluding that the brecciform rocks
- under review have resulted from the alteration of beds of conglome-
rate. The stones often look as if they had been squeezed while in
a softened condition. I have picked out two water-worn stones,
which appeared to have been flattened against each other ; and some-
times a somewhat rounded amygdaloidal stone would be found with
with a harder pebble partially squeezed into it, and strongly adhe-
ring. A few stones, all much of a size, seemed as if they had been
pressed together while in a softened state, and had thus assumed
regular hexagonal forms.

There are several other points of interest in connexion with these
brecciiform masses, especially as regards their relations to the green
paste-rock; but their consideration at present would involve too
much detail. In places where the original condition of the beds
has been closer-grained or finely comminuted, we may have areas
somewhat analogous to the pseudo-bombs of nascent amygdaloid:
these, by their union, go to form a compact felstone.

The coarser parts of Knockdolian rock also shade off into a simi-
lar hard compact shattered felstone—a result brought about by the
welding. or soldering together of the angular brecciiform frag-
ments*,

D. Finely Crystalline Felstones.

A large proportion of the felspathic metamorphic rocks consists
of finely crystalline and compact felstone. These rocks are well
exposed at various points along the coast to the north of Bennane
Head, but they are better seen upon the-whole in the interior of the
country, along hill-sides and in stream-sections, They seldom show

* Conglomerates in various stages of alteration have been examined in other

localities of the district, and will ‘be described in n the Memoir of the Geological
Survey to accompany the Map, sheet 7.

026 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

well-marked bedding; but occasional dips may be observed. Their.
general character is that of a shattered, close-grained, finely crystal-
line, sometimes compact rock, becoming coarsely crystalline and
even porphyritic in places. Passages from hardened granular grey-
wacké into semicrystalline rock, and from that into the close-grained
felstone, are of common occurrence. Not infrequently areas of
granular wacké may be obtained completely encircled by felstone,
both being evidently parts of the same bed; and, on the other
hand, portions of finely crystalline felstone make their appearance
in the midst of comparatively unaltered wackés. These are cer-
tainly not dykes, nor intrusive masses, but are merely meta-
morphosed parts of the beds among which they occur; for they
distinctly shade off into the semicrystallme and granular matter
which encleses them. They seem in this way to be analogous to
those vesicular areas so characteristic of some basic greywackes.
The greywacké beds which have been partially converted into com-
pact felstones are most usually fine-grained rocks with little or no
calcareous or magnesian matter ; and this insufficient supply of alka-
line matter probably accounts for the absence of amygdaloidal cavities.
Whenever the strata begin to get alkaline, the altered crystalline
areas become amygdaloidal.

When the strata have originally consisted of alternations of very
highly basic with less alkaline beds, the resulting metamorphic masses
exhibit a great variety of rocks. Thus on the shore at Lendalfoot
the sea-stacks and skerries show confused alternations of felstone,
felspar-porphyry, hardened granular greywacké, altered limestone,
hyperite, diorite, diallage-rock, serpentine, and occasional breecii-
form beds ; but although there is much confusion in detail, still, when
viewed on the large scale, the direction of the masses agrees with the
strike of the rocks of the district. The fine-grained felstones here-
abouts are remarkable chiefly as showing how felspathic rocks may
in places become diorites. In this metamorphic district no rigid
line can be drawn between the two, either by mineralogist or geolo-
gist. Near Lendalfoot the felstones are often thickly studded with
blotchy crystals of white felspar, which, being much harder than the
matrix, stand out in relief on weathered surfaces. These crystals
are aggregated in a very irregular manner. ‘They are of small size
where they are most abundant; but in the more sparsely porphy-
ritic areas of the felstone they are usually larger, being sometimes
an inch in Jength. Occasionally the beds show more or less distinct
crystals of hornblende, which increase in number until, by their
abundance, they impart a dark hue to the rock. This, then, we
should call diorite. But for fuller details 1 must again refer to a
forthcoming memoir of the Geological Survey.

III. Drorrric Rooks.

The dioritic strata do not occupy so large an area as the felspathic
rocks; they are also of more interrupted occurrence, frequently
appearing as small lenticular layers interstratified with serpentines,

1866. | J. GEIKIE—-CARRICK, AYRSHIRE. 527

but very rarely with felstones. The more extensive rock-masses
present very much the same contour as the metamorphic felspathic
strata, forming rounded hills and knolls with a somewhat lumpy
outline.
- Under the term dioritic are included all those rocks which consist
essentially of silicates of lime and magnesia set in a felspathic base
or matrix; but a description of the many phases presented by the
class of rocks referred to 1s beyond the scope of this communication.
They show every gradation of texture, from a rock nearly compact to
dioritic masses in which the crystals often exceed an inch in length.

The principal varieties are diorite and hypersthenite, both of
which are occasionally foliated. The felspar usually associated with
hornblende and hypersthene in these rocks is a hard white variety.
Diallage-rock occurs sparingly in one or two localities; sometimes a
well-marked diorite exhibits crystals of white and clear quartz, and
thus becomes a syenite.

Where the dioritic rocks are typically developed they are invari-
ably associated with serpentine. With this rock they exhibit inter-
esting junctions, to which reference will presently be made.

LY. Serpentine.

Serpentine rock abounds throughout the district; it consists of
two principal varieties—foliated or schistose, and compact.

1. Schistose Serpentine.—This is very plainly a bedded rock, and
is generally interstratified with diorites. It varies in colour from
reddish-brown to green. The folia correspond with planes of bed-
ding ; but in some places the foliation is rude and irregular, and,
in the absence of well-marked dips in adjoining crystalline and
gritty beds, cannot always be asserted to coincide with original
lamination. Vein-lke ramifications of diallage-rock, consisting of
masses of diallage-crystals, sometimes intersect the schistose varie-
ties of serpentine. The joints are often abundantly coated with
soapstone, chloritic matter, and other silicates of magnesia and
alumina.

2. Compact Serpentine.—This occurs in much larger masses. Dark
and pale green are its usual colours, but areas of red and beautifully
mottled green and red varieties are not uncommon. Sometimes it
is poryhyritic with diallage, and very frequently with bronzite.
Traces of bedding have seldom been observed in these rocks them-
selves; but the trend of the masses agrees with the strike of the
rocks of the district, and interstratified lenticular beds of diorite are
of common occurrence, thus showing that the compact serpentines,
like the altered strata with which they are associated, are truly bedded
rocks. The association of serpentine with limestone will be ad-
verted to presently.

A few notes upon the coast-section between Pinbain and Lendal-
foot may serve to throw some light upon the probable origin of the
serpentines of this neighbourhood. On the shore near Pinbain
occur some vertical beds of dark shales closely associated with a

528 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

spheroidal brecciiform rock similar to some of those described above.
These shales are often much twisted and broken, and are interstra-
tified here and there with interrupted bands of altered wacké, which
are also brecciated. There are many points of interest connected
with the brecciiform stones at this place; but these cannot be
considered here. The most notable feature about the beds is the:
occurrence of limestone in the shales. Among much disturbed and
brecciiform beds may be seen a large block of limestone, four feet
across. It looks as if it had been forcibly pushed into its present
position ; for the shales are all puckered and squeezed about it.
Many smaller calcareous fragments occur in its vicinity. In their
neighbourhood the beds are abundantly veined with carbonate of
lime; but these veins are chiefly confined to an irregular band
or area along the direction of the strike. There can be no doubt
that the veins have resulted from the dissipating, a situ, of a lime-
stone, they and the honeycombed and amorphous-shaped blocks
being all that now remain of that bed. A yard or two from
this point may be seen irregular nodular calcareous bands in
dark greenish shales, which are here much less disturbed. The
confusion observable in the former case must therefore in
great measure be due to the withdrawal of the limestone.
Leaving these shales and continuing the section southward we come
at once upon highly metamorphic strata, consisting chiefly of ser-
pentine with interbedded dioritic masses and occasional areas of
felspar-porphyry. The bed immediately associated with the dark
greenish shale is a serpentine ; but the junction, unfortunately, is not
well seen. There can be no doubt, however, that the schistose ser-
pentine is merely a metamorphosed shale. All serpentine-rock
contains less or more alumina, and many of the ophiolites of this
neighbourhood are in this way very impure; indeed it is often
impossible to distinguish between highly magnesian shale and
impure schistose serpentine. Geologically, the latter is only an
altered condition of the former. The veins of diallage which are
sometimes found in these shaly and schistose varieties may not
improbably represent calcareous veins similar to those that traverse
the dark shales alluded to above, subsequent metamorphic action
having converted them into diallage. The silica and magnesia
necessary to this change would, of course, be derived from the
impure magnesian rocks through which the veins ramify, and which
at the time the veins were forming were assuming their present ophio-
litic character. In like manner, the bronzite, especially in the more
compact serpentines, may partially represent the carbonate of lime that
was diffused through the rock before alteration began. Crystals of
bronzite and diallage are so abundant throughout large areas of
serpentine as frequently to form a jifth, and’ sometimes even a
third, of the bulk of that rock. The condition of the beds before
metamorphism ensued may therefore have been that of impure or
muddy dolomitic or magnesian limestones. In support of this view
it may be mentioned that, in less altered areas of the district,
limestone has been met with which was sometimes magnesian.

1366. ] ‘J, GEIKIE—-CARRIOK, AYRSHIRE, 529

Of course it may be said that this magnesian character has been
superinduced by metamorphic action. Perhaps it has; and if the
process of alteration had been continued, we might have had
serpentine in place of an impure magnesian limestone. We must
suppose that metamorphism is a gradual operation, and that the
rocks acted upon assume various characters as the action proceeds,
Serpentine is evidently an advanced stage in the process.

3. Association of Diorrte and Serpentine.—The junction between
serpentine and diorite is often very distinct; but in other places
where the latter is fine-grained and highly magnesian, it passes so
insensibly into the former that we are frequently at a loss to tell at
what point we must cease to call the rock a diorite, and when we
ought to begin to describe it as serpentine*. In cases of this kind
we may reasonably infer that the original composition of the beds
which has given rise to the diorites shaded gradually into that of
those more highly magnesian beds whose metamorphism has re-
sulted in serpentine. On the other hand, when the junction between
that rock and diorite is well marked, it appears probable that the
composition of the various strata before metamorphic action began
was also well marked, one bed not shading off into another as in
the previous case. :

A few notes on the better-marked junctions of serpentine with
diorite may be interesting. As it approaches diorite, serpentine
frequently becomes rudely schistose and sometimes quartzose—so
much so that it might occasionally be described as a highly silicated
felspathic schist, tinged green with magnesian matter. Here, also,
it sometimes shows irregular interrupted bands of yellow, green,
and brown Lydian-stones. The junction with the diorite is very
irregular, the serpentine appearing as if it had been caught up
every here and there, while occasionally long branching fingers of
magnesian matter are protruded into the diorite. Small veins of
diorite, also, in some cases pass into the serpentine. It is, no
doubt, appearances of this kind which in some cases have led geolo-
gists to consider serpentine as of igneous origin. On the sea-shore
at Lendalfoot many excellent junctions of the nature alluded to may
be studied. The strata at this place are very much confused;
nevertheless alternations of serpentine with diorites and felstones
succeed each other in such a way as to indicate that we have here
the original bedding.

VY. Luesrone.
It now only remains to add a few words about the limestonest

- * On the hills a little to the north-east of the village of Colmonell (river
Stinchar) a very peculiar serpentine occurs. Interspersed throughout a base
of dark-green serpentine (which in places is porphyritic with bronzite) abun-
dant granules and interrupted nodular threads of white felspar make their
appearance. The matrix in which this felspar occurs is harder than the other
-portions of the rock, where the serpentine presents its normal character. As
this peculiar rock certainly passes into diorite (hornblende and felspar) there can
be no doubt that the hardening of the green serpentinous matrix is due to the
presence of lime in chemical union with the silicate of magnesia. .

t These limestones haye yielded fossils of Lower Silurian age, a list of which

530 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

and calcareous wackés. These, as we should expect, are of very
limited extent. They never continue any distance, but speedily
give way in all directions to metamorphic rocks. The limestone of
Craigneil is a remarkable example. The hard and tough nature of
this rock has enabled it to withstand denudation better than the
more easily wasted conglomerates and altered wackés by which it is
surrounded. It rises into a conical hill, the form of which is eyi-
dently due to glacial action. Although this bed is of considerable
thickness, it yet dies out very suddenly along the strike ; and the same
appears to be the case with the limestone at Bougang. Of the
Craigneil limestone itself not much need be said here, further than
that it is a very impure rock, and ought in places to be termed
merely calcareous greywacké. It is associated on the south side
with schistose serpentine and conglomerate. To the west and east
it is replaced by altered, crystalline and amygdaloidal greywackés.

Association of Serpentine with Calcareous Strata.—At Laffin-
cleary, serpentine is curiously associated with a highly calcareous
wacké and impure lmestone. The serpentine occurs as veins and
amorphous areas, and is itself veined with carbonate of lime. The
calcareous beds have in places assumed the brecciiform structure of
Knockdolian reck. On the old raised beach at Whilk, at Bennane
Head, at Leffin Knowes, on the farm of Balnowlart, on Knockdolian
Hill, in an old quarry at Bougang, at Knockdhu Bridge, and many
other places, limestone or calcareous wacké is found abundantly
intermingled with magnesian matter, and occasionally passing into
serpentine. The rock is generally much confused and broken, the
joints being coated with such silicates as steatite, chlorite, &e.

These calcareous areas are, as remarked, always of small extent,
and occur quite sporadically, often with no apparent relation to each
other. But occasionally they seem to follow a certain line corre-
sponding to the direction of the strike. Little patches of serpentine,
in the same manner, often make their appearance at intervals on a
given horizon. Whether these last indicate the former existence of
impure magnesian and caleareous wackés or limestones, like the
sporadic beds just referred to, can only be conjectured.

With regard to the former extent of such limestones as those at
Craigneil and Bougang not much can be said. Metamorphic action
has in all probability considerably reduced their bulk; but there are
good grounds for believing that they never covered any large con-
tinuous area, but, on the contrary, were from the first of partial and
irregular occurrence.

VI. Conctiuston.

In the foregoing general sketch of the phenomena of this inter-
esting region, speculations on the probable nature of the agent or
agents by whose means the alterations were effected have been pur-
posely omitted. It is usually much easier to say what has not
caused such changes than to state what has; but in the present

will be found in Sir Bote Murchison’s memoir already | gests to. Kide
Quart. Journ. Geol. Soc, vol. vii. p. 154.

1866.] J. GEIKIE—CARRICK, AYRSHIRE. 531

instance, at least, there can be little doubt that the metamorphism
ought to be assigned to hydrothermal action. The very partial
manner in which the strata have been affected—the frequent occur-
rence of unaltered areas among crystalline rocks and vice versd—the
various degrees of intensity which characterize the metamorphism,
even when the beds undergoing change have much the same compo-.
sition—all seem to point to the partial distribution of moisture or
water in the strata at the time metamorphic action ensued, so that
when heat began to attack the beds, its influence was aided in a
greater or less degree by the amount of water present in the rocks.
The probable source of this water will be considered presently.

Many portions of the strata have merely undergone a process of
hardening, which has sometimes given to the beds a semicrystal-
line texture—a change which ei be brought about without fusion
or softening. But the appearances presented in some places require
us to infer a former pasty or almost semifluid condition. It is un-
necessary to recapitulate the evidence on this head; but reference
may be made to a few of the facts already adduced.

The phenomena connected with isolated amygdaloidal areas are
especially worthy of study. ‘The little cells have attained their
spherical shape at a time when the matrix had a certain plasticity.
If this plasticity had been caused by dry heat, it is difficult to
understand how the granular portions of the same beds should have
escaped change, especially as their composition does not differ from
that of the amygdaloidal areas. The whole series of phenomena
associated with the gradual increase of separate amygdaloidal areas,
and the progressive formation in this way of spheroidal and colum-
nar amygdaloid, appear explicable only on the assumption of hydro-
thermal action.

The appearances presented by felspar-porphyry seem to bear out
the same view. Nothing is more striking than the often close
association of highly metamorphic with comparatively unaltered
areas. Greenish granular wacké has been observed so close to fel-
spar-porphyry that only a thin irregular ribbon of rudely schistose
serpentinous matter kept the two rocks from touching. It was in
this wacké that isolated vesicular areas were first detected; so that,
although the beds retain in great measure their granular structure,
yet they cannot be said to be quite unaltered. But that they should
have experienced so little change in the immediate vicinity of a
rock the nature of which evinces great intensity of metamorphic
action is not a little surprising. It is not improbable, however,
that the felspar-porphyry, having been reduced to a soft-or viscous
state, has been partially forced out of its position by the weight of
superincumbent strata pressing upon it, and in this way intruded
among other rocks which had not undergone the same degree of
change. Of the truly metamorphic origin of the felspar-porphyry
there can be no doubt. Its behaviour at other points has been
referred to above.

Of the stones of the brecciiform rocks or altered conglomerates, it
was remarked that they are for the most part of angular and sub-

532 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

angular shapes, but often with a general approach to roundness,
especially when imbedded in a matrix. The whole aspect of these
stones forcibly suggests hydrothermal action. In many places the
pebbles have been mutually squeezed, so as to become distorted, and
sometimes to assume hexagonal forms, thus implying a somewhat
softened condition*.

Without going into more detail, allusion may be made to an inter-
esting point in connexion with certain metamorphic rocks of Lower
Old Red age, belonging to another district of Ayrshire, situated
some miles to the north-east of Girvan, on which the Survey
was engaged during the past year. The rocks of this district are
chiefly felspathic varieties, and present very much the same phe-
nomena as has been shown to characterize the altered felspathic
wackés of the Silurian strata. Near the farm of Knockdon, on the
Water of Girvan, occur conglomerates and felspathic sandstones
which have been converted in places into dark and light pink fel-
stones. Many portions of these felstones were found to be porphy-
‘ ritic, often abundantly so, with fan-like radiating fibrous erystals of
a dark greenish zeolite. Sometimes the same mineral oceurred in
amorphous blotches. These zeolites did not fill up amygdaloidal
cavities, but were in every way analogous to the porphyritic crystals
of a felspar-porphyry. We must therefore admit that, in some way
or other, water has had to do with the production of these meta-
morphic felstones.

The nature and origin of the veins which traverse the metamorphic
Silurian rocks of Carrick afford very strong support to this con-
clusion. I cannot enter here into the evidence which goes to prove
that the thick ramifying veins of carbonate of lime, diallage, felspar,
zeolite, d&ce., are all of the same age as the metamorphism, and are not
due to subsequent infiltration. Veins of carbonate of lime have been
described as proceeding from imbedded blocks of limestone ; knotted
strings of diallage crystals have been pointed out as forming part of the
bed in which they occur; veins of felspar are associated with ex-
ceedingly coarse diorite in such a way as to show that their origin
must be contemporaneous with that of the diorite ; while abundant
veins of a beautiful white fibrous zeolite, that traverse the strata in
many places, are also to be assigned to the date of the general
metamorphism. Mr. Richard Smith, of the Geological Museum,
Jermyn Street, kindly undertook the analysis of this zeolite, the
composition of which he ascertained to correspond with that of
pectolitey.

* But such distorted stones must be carefully distinguished from the appear-
ance presented by a fine-grained semicrystalline felspathic rock which seems to
be entirely made up of little rounded pellets like pebbles. This, however, is a
superinduced structure. ‘The pellets vary from the size of peas to that of hazel-
nuts. When they press closely, they frequently become five- or six-sided. It is
difficult to account for this peculiar structure; but that it has been induced by
hydrothermal action, and not by dry heat, is borne out by the testimony of the
surrounding metamorphic phenomena. :

+ Since Mr. Smith’s analysis was made, I find that pectolite had been
obtained by Prof, James Nicol from the same neighbourhood.

1866. ] J. GEIKIE—CARRICK, AYRSHIRE. 533

Assuming that the metamorphism of these strata has been mainly
effected by hydrothermal action, a word or two may be added re-
garding the probable source from which the water has been derived.
All rocks are found to contain a variable amount of water; but the
strata nearest the surface of the earth are, for the most part, better
saturated with moisture than the beds at lower depths. The supply,
when derived from rains and the water of springs, rivers, and lakes,
must from various causes be very partially distributed. If, there-
fore, the intensity of metamorphic change be influenced by the
amount of water present in the rocks, we should expect to find
the strata often showing sporadic areas of alterations. Nor need we
be surprised when metamorphic beds occur superimposed upon less
metamorphosed and unaltered rocks. With regard to wide regional
metamorphism, like that of Canada, the Scottish Highlands, and
Norway, it is probable that the strata acquired their metamorphic
character while they lay underneath the bottom of the sea. During
such a period or periods of submergence, water could not fail
to find its way into the subjacent rocks, down through which it
would continue to percolate until it reached a point where the con-
ditions of heat might enable it to attack the strata and gradually
effect their metamorphism. ‘The action of the heated water would
doubtless be often aided by the chemical reagents it held in solution,
and the ultimate character of a metamorphic rock might not infre-
quently depend upon the nature of such acid and saline solutions.
But the present aspect of the Carrick metamorphic rocks, at all
events, is certainly not due to this cause alone, but chiefly to the ori-
ginal composition of the unaltered strata. The elements necessary to
the formation of diorites and felstones were not introduced by water
during the process of alteration, but already existed in the beds
before metamorphic action began.

On the hypothesis that the water necessary to hydrothermal
action has been supplied in the manner indicated, we can under-
stand how the lower beds of the Silurians of Carrick have escaped
alteration ; for either the water percolating downwards never pene-
trated so far, or else was present in too small quantity to induce a
wide-spread change. It is quite consistent with the views sup-
* ported above, to suppose that during its downward passage the
water may have been deprived of certain chemical reagents before it
reached great depths, so as in some measure to have become
weakened, and thus less capable of affecting the condition of the
strata. When its passage, however, was aided by jointing and
fractures, it might occasionally sink to great depths, and there give
rise to metamorphic action. In this manner, we may account for
those isolated areas of crystalline rock that occur among the un-
altered strata, on a lower horizon GE the chief metamorphic
masses.

The only i igneous rocks of the district are a few dykes of felstone
and greenstone, which are evidently of much later date than the
metamorphism. The granular wackés through which they pass.
usually remain quite unaltered, even at their immediate junction with

534 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

the trap. Nor is there the slightest evidence of the existence of
any underlying mass of igneous rock, the heat of which might be
supposed by some to have caused the alteration of the strata. In the
second metamorphic area to which I have had occasion to refer,igneous
rocks are largely developed; but, curiously enough, the most highly
altered strata occur at a distance from the intrusive traps. The
rocks immediately surrounding one large mass of felstone, about a
mile and a half in circumference, were for the most part quite
unaltered. They consist of conglomerates and chocolate-coloured
sandstones and grits. But outside of this unaltered area, felspathic
erits and sandstones have become felstones, and conglomerates
have been in places changed into bright-pink and fawn-coloured
porphyry. We cannot, therefore, consider intrusive trap to haye
been the source of heat in the metamorphic areas referred to, and
must thus accept the theory, so ably supported by many geologists,
that the temperature necessary to metamorphic action has been
derived from the central heat of the earth.

The facts advanced in the foregoing communication seem to
rove :—
i Ist. That the strata owe their metamorphism to hydrothermal
action.

2nd. That the varying mineralogical character of the rocks is
due principally to original differences of chemical composition, and
not to infiltration of foreign matter at the time of metamorphism.

ord. That the highly alkaline portions of the strata have been
most susceptible of change.

Ath. That in beds having the same composition, but exhibiting
various degrees of alteration, the intensity of the metamorphism has
been in direct proportion to the amount of water passing through
the strata. .

5th. That in some places the rocks have been reduced to a softened
or pasty condition.

3. On a CHELROTHERIAN Foorprint from the Basz of the Knurrr -
Sanpstone of Darespury, CuesHire. By W. C. Wirziamson, Esq.,
F.R.S., Professor of Natural History, Anatomy, and Physiology
in Owen’s College, Manchester.

[Communicated by the Assistant-Secretary.4
(The publication of this paper is unavoidably deferred.]

[ Abstract. ]

THE specimen in question was discovered by Mr. J. W. Kirkham, in
the Lower Keuper Sandstone at Daresbury Quarry. It differs from
all footprints hitherto obtained from this district, in being more
quadrate, and distinctly that of a scaly animal; the separated toe is
also less recurved, and approaches nearer to the other toes, The

1866. ] PIKE—‘“' HEAVES”” IN PENHALLS MINE. 595 15)

arrangement of the scales corresponds very closely with that seen in
the foot of the living Alligator; many of them run across the foot in
oblique lines, as is common amongst living Crocodilians, leaving no
room to doubt that they represent true scales, and not irregular
tubercles, such as are seen on the skin of some Batrachians. Traces
of other impressions of feet occur on the slab, particularly an im-
perfect one with much larger and more oblong scales, especially under
the heel; and this difference is so very similar to what is seen in the
fore and hind feet of many Saurians, that Prof. Williamson believed
that they did not belong to a Batrachian animal at all, but that they
were Saurian, if not Crocodilian, in every feature.

4, A Description of some remarkable “ Huaves” or Torows in
PrenHALLs Mine. By J. W. Pixs, Esq.

(Communicated by C. Le Neve Foster, D.Sc., B.A., F.G.S.)

THis mine is situated in the parish of St. Agnes, in the county of
Cornwall, and stands on the sea-coast, three or four hundred yards
from the edge of a bold precipitous cliff rising to a height of 300
feet above the sea-level.

Pryce, in his valuable old book ‘ Mineralogia Cornubiensis,’ and
Carne and Hawkins in papers read some forty years ago before the
Royal Cornwall Geological Society, together with many other writers,
refer to the heaves of the celebrated Pink lode, which is now a part
of Penhalls Mine.

A paper was also read in 1815 before this Society, by Mr. John
Williams, entitled ‘“‘ Account of some Remarkable Disturbances in the
Veins of the Mine called Huel Peever,” the appearance of the
lodes in which mine present the nearest approach to the dislocations
in the Penhalls district.

The nature of the ground or “ country ”’ is a light-grey, distinctly
stratified “ killas” (the clay-slate of many geological writers, though
not a cleaved rock) with a pretty regular dip towards the north of
from 20° to 25°.

In the immediate neighbourhood of the workings the ground is
traversed by :—

1. Four or five tin-lodes, varying from 4 feet to a few inches in
width, dipping north at about the same angle as the killas, and com-
posed of the oxide of tin, with a little iron and copper pyrites in the
middle,—the walls or outsides, locally called capel, being a hard grey
killas with quartz and schorl. The only distinction between the
different lodes is in the appearance of the tin-stone, which varies in
the size of the grain and in colour.

2. Three or four ‘‘ downright” lodes averaging a foot in width
and running east and west. Their composition is something between
the tin-lodes and the “ gossans ;” indeed in depth they generally
decrease in size and pass into gossans.

3. Numerous “ gossans’’* (lodes or veins), varying from a few

* A gossan in most parts of Cornwall consists very largely of an ochreous
VOL, XXIT.—PART I. 0

536 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 6,

inches to 3 feet in width, running somewhat about east and west,
dipping, although mostly south, at various angles, and composed of a
“voughy”’ or cavernous quartz, with crystals often coated with
brown iron-ore, and copper and iron-pyrites. They often present a
very irregular appearance, being split up in small branches.

4, A great number of “ slides” or faults, of from 3 inches to a
foot in width, dipping at various angles, and mostly with an east
and west bearing. There are some, however, called ‘“ caunting”
slides, running north-east and south-west. They are formed, no
doubt, by the dislocations of the adjacent “country,” consisting
as they do of decomposed killas, as if the rock had been ground
together and then acted on by water.

Lastly. Four cross courses (north and south veins), one only of
which is of any consequence. It averages 34 feet in width, -is
nearly perpendicular, and is filled in with decomposed killas and
masses of quartz.

The influence which these lodes and veins exert on each other
will be seen in the transverse sections (figs. 1 & 2),—the tin-lodes
(that is, Cowling’s) and the Flat lode being thrown by the “‘ down-
rights,” gossans, and slides, the ‘‘ downrights” by the gossans and
slides, and the gossans by the slides, although there does not happen
to be an example in the section of the latter case. A southern
dip in the traversing vein throws the lode traversed up in going
from 8. to N., and a perpendicular or northern dip depressing it ;
in other words, the “ hanging wall ” of the traversing vein seems to
have moved down, or the “ footwall” to have moved up—the wider
the traverse the further. the heave. The cross course masters all the
east and west veins, throwing them to the right hand a distance of
from 20 to 30 fathoms, the tin-lodes being thrown further than
those of more recent formation. The cross courses, however, have
to yield to the “caunting” slides, as seen in an adjoining mine,
which throw them a little on the side of the acute angle. The
mineral productiveness of the tin-lodes is increased by the proximity
of the gossans, but not by that of the slides. 7

As before stated, the dip of the “country” is generally pretty
regular ; yet still very marked evidence of disturbance can easily be
perceived in some places, the line of stratification presenting a very
wavy form. This is especially seen sometimes near the gossans
and slides, where, at the immediate point of junction, the beds of
killas are found to bend up on one:side and down on the other,
affording additional proof of the direction of the heave. The relative
ages of all these veins may be at once determined from the above
facts. Taking the well-known law, that a lode or vein traversed is
older than the one traversing it, as a guide, we shall have :—

1. Tin-lodes. | 4. Kast and west slides.
2. “Downrights.” 5. Cross courses. |
3. Gossans. 6. ““Caunting”’ slides.

Slides, according to Carne, are generally considered to be of more

brown iron-ore. At St. Agnes the meaning attached to the term is somewhat
different. ae es

1866.] ' PIKE—‘‘ HEAVES ” IN PENHALLS MINE. 537

recent formation than cross courses ; but in this district the contrary
seems to be the case in those of an east and west bearing. It is
needless to state how perplexing these “ Will o’ the Wisp” kind of
lodes are to the miner, no sooner being found than lost ; and although
he may generally be able to tell which way to turn to regain them,
yet still they have often been acted on by so many conflicting in-
fluences that he is sometimes at a loss how to proceed.

An instance of this complication can be seen in the section (fig. 1)
in the engine-shaft, a little above the 50-fathoms level, where a
downright, No. 2, acts on Cowling’s lode, throwing it down, but just
misses the flat lode, which is caught by the slide and thrown up.

Fig. 1.

Cowlings lode ......
Piablode .s....c0....
Downright, No. 1.
Downright, No. 2.

50 fm. level.

Engine shaft.

Fig. 2.

Down right...
North lode... a=
Gosgan.......+»

—

iy
1 iN
ANH
Din Seac<

rs
>
&
&

The district has nevertheless yielded great riches, and has been
worked from time immemorial.

538 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

JunE.20, 1866.

The following communications were read :—
1. On the Structure of the Rep Crac. By 8. V. Woon, F.G.S.

Mr. Presrwicn has, I believe, for several years inclined to the
opinion that the Red and Fluviomarine Crags are coeval; but, so
far as I am aware, he has not expressed that opinion in print. In
1863 my son had arrived at a similar conclusion; and in a paper
by him, published in the ‘ Ann. & Mag. Nat. Hist.’ for March 1864,
he showed that the Chillesford beds overlie alike both the Red and
Fluviomarine Crags, and that the Red Crag itself was not all of
one age, but divisible into distinct portions, the uppermost of which
he regarded as newer than the Fluviomarine, and intermediate 1 in
age ponnece it and the Chillesford beds.

In December 1864 another paper by my son was read before this
Society (but was afterwards withdrawn, and an epitome of it,
together with a map of the Upper Tertiaries of the East of England,
printed for private circulation), wherein he contended that the so-
called Weybourne Crag, the Cromer Boulder Till, and the Contorted
Drift formed a separate series, to which he ‘assigned the term
“ Lower Drift,” and that this a common with the Red and Fluvio-
marine Crags was overlain by the great body of sands which inter-
vene between the Crag and the Boulder-clay, and to which he ap-
plied the term ‘Middle Drift,’ distinguishing the Boulder-Clay as
the “Upper Dnft.”

In November 1865 a paper, by the Rev. O. ‘Fisher, was read
before this Society (and published in their ‘ Quarterly J ournal,’ Feb.
1866), wherein he impugns the position of superiority which had
been given to the Chillesford beds, and assigns their position in the
following descending order:—I1st, Fluviomarine (Norwich) Crag ;
2nd, Chillesford Clay; 3rd, Mya-bed beneath the Clay; 4th, Red
Crag.

In this state of things I determined with my son to reexamine
the whole country between Woodbridge and Easton Bavent Cliff;
and the result of that examination appeared to show the undoubted
superiority of the Chillesford beds to the Fluviomarine Crag in the
case of the pit at Thorpe, near Aldborough, as also in the pits at Bul-
champ and Wangford.

In the first place I examined and collected from the shell bed at
the foot of Easton Cliff, and also in the pit found by Mr. Fisher at
Yarn Hill. I quite agree with that gentleman that it is exactly
the same bed as that in the micaceous sands discovered at Chillesford
by Mr. Prestwich and others in 1849, and which Mr. Fisher
designates as the Mya-bed,—the only difference being that the
Easton and Yarn Hill development of it points to a somewhat
estuarine character, by the absence of Mya truncata, so common in
it near Chillesford, and by the substitution for that shell of Mya
arenaria—a feature which the Yarn-Hill and Easton bed shares
with what (as my son informs me) is identically the same bed,
recently discovered by Mr. Rose at Toft Monks, on the Waveney,

1866.] i WoOD—RED CRAG. 539

opposite Beccles. The shells which Mr. Rose has collected from
this place (of which he has kindly sent me a list), with those
collected by myself and Mr. Fisher at Chillesford and at Easton
and Yarn Hill, now furnish a tolerably complete fauna of this
formation.

The only pits of the true Fluviomarine or Norwich Crag (so far
as my knowledge goes) that exist in Suffolk are three—-one at
Thorpe, near Aldborough, another at Wangford, and the third at
Bulchamp. In the case of the first, although there is no evidence
of oblique bedding, the bed dips at an angle of 7° or 8°, and I have
no doubt that a slight fault or upheaval has taken place, bringing
the Crag to the surface at this one point only, which is at some
height above the base of the contiguous cliff at Thorpe. On the
opposite side of the railway, however, and upon the top of the hill,
occurs a pit of the Chillesford Clay. The bed is unmistakeable ;
and, as one stands at the edge of the Clay-pit, the Crag is visible,
in the hollow below, at a distance of about a quarter of a mile, so
that one may look down from the top of the Chillesford Clay, some
20 or 25 feet, on to the Crag exposed in the other pit (see fig. 1).

Fig. 1.—Section showing the position of the Thorpe Crag-pit
relatively to the Chillesford Clay (3 furlongs).

W.S.W. E.N.E,
Clay-pit,5 furlongs —
E.N.E. of Aldring- Railway- Thorpe
ham Church. cutting. Crag-pit,

b. Chillesford Clay. marine Crag and Chillesford Clay
c. Red sands between Fluvio- | (d3' & 4' of Diagram).
d. Fluviomarine Crag.

A little south of the line joining the two occurs a pit of red sand,
‘belonging, as I consider, to the sands intervening between the
Norwich Crag and the Chillesford Clay; the railway-cutting, a
furlong still further south, is in the same sands. This is the pit in
which Mr. Fisher says Mytsi occurred, and which he regards as
immediately underlying the Boulder-clay; the sands, however, I
consider to be those intervening between the Thorpe Crag and the
Chillesford Clay.

The Crag in the pit at Bulchamp, which is a few feet above the
marshes of the Blyth, has, like the Thorpe pit, been subject to some
disturbance, bringing it to the surface at this place only; for in
none of the pits in the red sand around at the same level does the Crag
appear; but in a pit about 2 furlongs to the north the Boulder-clay
has been let down beside the red sand by a vertical throw, which,
calculated from the place of the Boulder-clay on the neighbouring
hills, cannot be less than 40 or 50 feet. No pit of Chillesford
Clay now remains open near enough to this to show a satisfactory
section.

540 PROCEEDINGS OF THE GEOLOGICAL socrery. [June 20,

At Wangford the Crag is at the surface continuously for about a
furlong, at the bottom of a hill, and comes out with the red sands over
it immediately above some marsh-ground. On the opposite side of
the valley, divided from the Crag by this marsh, a Chillesford-Clay-
pit occurs, on the top of the hill, distant about half a mile, occupying
precisely the same position relatively to the Crag-pit as does the
Chillesford-Clay-pit at Thorpe to the Crag-pit there (see fig. 2).
Were it not for the interception of the view by a row of high trees, a

Fig. 2.—Section showing the position of the Bulchamp and Wangford
Crag-pits relatively to the Chillesford Clay (2 miles).

1 Ge
oa be £ wy ce N.E.
: ae : S
ea ae Face eae B58 gE Es
, Se Bees ces ashes SB
e Ba nee ses a aa ZB Pk
ei mo H5HE O%6 Red-sand- § 235 a eS
a as Fan pits. oem SES
H ' 1 i H 1
bes | ib Werk
(yy K ms H !
2 |

{free wise oom ene mena =~

a. Boulder-clay. Crag and the Chillesford Clay
6. Chillesford Clay. _ (d3' and 4' of Diagram).
e. Red sands between Fluviomarine | d. Fluviomarine Crag.

spectator standing on the edge of the Clay-pit here would look down
into the Crag-pit some 20 to 25 feet below him, in the same manner
as is the case at Thorpe. Nothing but an actual vertical section
(which would require to be 30 feet at least in height) could, I think,
show more clearly the superiority, in these places, of the Chillesford
Clay to the Fluviomarine Crag than do these two sections. With re-
spect to the passage upwards of both the Fluviomarine and Red Crags
into the Chillesford beds, it is only necessary to observe that there
is nothing to indicate any break either physically or palzontologically.
In the case of the Fluviomarine Crag the interval is represented by
a mass of red sand, of which abundant sections occur around Wang-
ford and Bulchamp, and which, as I have said, is in section at the
Mytilus-pit of Mr. Fisher at Thorpe, and in the adjacent railway-
cutting. The sand containing the shell-bed, which passes evenly
into the Chillesford Clay, and shells of which occur in the base of the
clay itself in the Cliff at Easton, is, I have no doubt, only the upper por-
tion of these sands; but no sufficient section seems to exist to show
the passage. In the case of the Red Crag this interval of sand is,
as my son pointed out to me, occupied by the upper or horizontal
portion of the Red Crag, exposed in the pit below the church at
Chillesford—that to which I have further on to refer as the Scrobi-
cularia-crag ; but neither of us could form a positive opinion whether
or not this Crag had been laid dry in the interval between its
deposit and the overspread of the sand containing the Chillesford
shell-bed (Mya-bed of Fisher). Pot-holes descend into it, but it is
not altogether clear whether these are of the age of the sand, or of
post-glacial origin; the even bedding of the sand over them seems,
however, to point to the former. Be this as it may, I do not regard

1866. | 3 WOOD—RED CRAG. 541

the break, if break there be, as anything more than the laying dry
for a short period of the shoal-deposit of the Scrobicularia-crag prior
to the overspread of the sand, and I now adopt the view expressed
by my son that the horizontal Crag which rests on the oblique at
Chillesford, “and underlies the Chillesford beds, and which has
always, and I think rightly, been regarded as part (although it be
the uppermost part) of the Red Crag, is newer than the true
Norwich or Fluviomarine Crag of Thorpe and Wangford.

The paleontological aspects presented by the Red Crag, however,
are the principal objects to which I desire to call attention, as
affording evidence of one of the most rapid changes in a fauna, when
measured by the vertical thickness of the beds furnishing it, that
geology affords; and as the most convenient and concise way of
representing the beds between the base of the Crag and the Boulder-
clay, to the lower portion of which my observations refer, my son
has prepared the annexed diagram, with a list of the various sections
from which it results, embodying the succession and relationof these
various beds according to his latest researches (see pp. 548, 549).

In the case of the Coralline Crag, we have evidence that it contains
the exuviz of animals the most removed from our own marine fauna,
in the fact that in it are the remains of 27 genera that are extinct
in the British seas :—

xCultellus. Nucinella. *Pleurotoma.
*Panopeea. Hinnites. Cassidaria.
Pholadomya. Lingula. Terebra.
Coralliophaga. Orbicula. xColumbella.
Chama. Sigaretus. Triton.
xCardita. *Pyramidella. Pyrula.
Verticordia. Fossarus. x Voluta.
Erycinella. xCancellaria. Ditrupa.
xScintilla. *Ringicula. Cleodora.

The genera marked with an asterisk are represented at Walton-on-the-Naze.

From this it is fair to infer that this Crag belonged to a period long
antecedent to the deposition of the Red. Indeed so far as the word
“Crag” indicates any material affinity between the two formations
it misleads, since, remote as it is, and severed from the present time
by a considerable sequence of deposits and events, the oldest part of
the Red Crag is less removed, palzontologically, from the present
time (and far less so from the Chillesford beds) than it is from the
Coralline Crag thus associated with it in name, but dissociated from
it in fact. The Red Crag, on the other hand, contains within itself
the evidence of a transition by stages, from the oldest, where its affi-
nities were to some extent with the coralline, and in a greater extent
with the existing Mediterranean, to its newer stages, in which the
shells are very few and confined to types peculiarly northern. Of these
stages the oldest and best-marked is that of Walton-on-the-Naze:
this Crag contains a fauna presenting a facies strongly indicative of
an origin or connexion with more temperate seas; and although there
is an absence from this bed of not less than 17 of those 27 genera
before mentioned as belonging to the Coralline Crag (a few of which
may perhaps be due to difference in depth of deposition), still the

542 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

presence of such species as Ovula spelia, Natica millepunctata, Tapes
texturatus, and Cardita corbis, now found only in the Mediterranean,
gives a presumption that the seas which deposited these fossils were
older than any other parts of the Red Crag. But the aspect of this
portion of the Crag is not more marked by the presence of such
forms as these, than it is by the entire absence from it of those
species whose connexion is now with the colder regions of the north,
such as Panopea Norvegica, Tritoniwm antiquum (dextral var.), Leda
lanceolata, and others; and it may be more especially remarked that
in the Walton Crag there has not been obtained a single unequivocal
specimen* of any species of the genus T'ellina, while the shells in
the upper beds of the Red Crag are composed mainly of individuals
of one or other of the species of that genus.

List of Species of Mollusca from the Crag at Walton-on-the-Naze.

(a denotes abundance.)

UNIVALVES.
Ovula spelta, Linn. - Cerithium tricinctum, Brocchi.
Cyprza avellana, J. Sow. Turritella incrassata, J. Sow.
Europea, Mont. Aporrhais pes-pelicani, Linn.

mat Anele ha. Sow., var. ?
Voluta Lamberti, J. Sow.
Columbella sulcata, J. Sow.

Nassa conglobata, Broc.

elegans, Leathes.

granulata, J. Sow.
propingua, J. Sow.

reticosa, J. Sow.

Buccinum undatum, var. striatum.
a. Buccinopsis Dalei, J. Sow.

Pyramidella leviuscula, S. Wood.
Eulima polita, Linn.

Leptoxis? terebellata, Nyst.
— ? pendula, S. Wood.

? suboperta, J. Sow.
Trochus cinerartus, Linz.
cineroides, S. Woed.
ziziphinus, Linn.

papillosus ?, Dacosta.
subexcavatus, S. Wood.

Odostomia unidentata, Mont.

a. Purpura tetragona, J. Sow. —— Adamsoni, Payr.

- lapillus, Linn. a. Natica catenoides, S. Wood.
Murex tortuosus, J. Sow. a. hemiclausa, J. Sow.

a. Tritonium antiquum, var. contrarium, helicina, Broce.
buccinatum ? a. —— multipunctata, var.
costiferum, S. Wood. millepunctata

Trophon muricatum, Mont. Capulus Ungaricus, Linn.

Mangelia Boothii, Smith. obliquus (Piliscus ?).

cancellata, J. Sow. militaris, Mont.
- levigata, Phil. Calyptrza chinensis, Linn.
mitrula, J. Sow. Tectura virginea, Mill.
- turricula, Mont. Emarginula fissura, Linn.
Cancellaria coronata, Scacchi. Fissurella Greeca, Linn.
Cerithium variculosum (lima ?). Actzeon Nox, J. Sow.
granosum, S. Wood. Conovulus pyramidalis, J. Sow.
BIVALYES.
Anomia, sp. Lima exilis, S. Wood.
Ostrea edulis, Linz. —— Loscombii, J. B. Sow.
Pecten opercularis, Linn. Mytilus edulis, Linn.
pusio, Pennant. Modiola barbata, Linn.

—— tigrinus, Mi//.

costulata, Rzsso.

* There is one specimen of TZ. pretenuis in my cabinet with the locality of
Walton attached, but it is of so old a date that I have now no recollection of it.

1866.]

WOOD—-RED CRAG.

BIvaLves (continued).

Modiola marmorata, Forbes.

|

a. Pectunculus glycimeris, var. sub- |

obliquus.
Arca lactea, Linn.
Nucula levigata, J. Sow.
Kellia suborbicularis, Mont.
Scintilla ambigua, Vyst.
Montacuta bidentata, Monz.
Lucina borealis, Linn.
Cardium edule, Linn.
Parkinsoni, J. Sow.
—— yenustum, S. Wood.
Cardita (senilis) sulcata?
scalaris, Leathes.
corbis, Philippi.
Astarte Basterotii?, Lajonk.
incrassata, Broc.
crebrilirata, S. Wood.
—— gracilis?, Miinst., var.

Venerupis Irus, Linn.
Cytherea rudis, Polz.
Venus fasciata, Dacosta.
—— imbricata, J. Sow.

. Artemis lentiformis, J. Sow.

lincta, Pulteney.
Gastrana laminosa, J. Sow.
Tellina crassa, Penn.
Abra alba, W. Wood.
fabalis,? S. Wood, var.
Mactra arcuata, J. Sow.
truncata, ? ovalis.
deaurata, Turt.(fide J. Brown).
Solen gladiolus, Gray.
ensis, Linn.
Cultellus tenuis, Phi.
Cochlodesma complanatum,
S. Wood.
Pandora pinna, Monz.

Corbula gibba, Olivi.
Corbulomya complanata, J. Sow.
Panopeea Faujasii?, Mén. dela Groy.
Saxicava rugosa, Linn.

a. Pholas cylindrica, J. Sow.
—— crispata, Linn.
Terebratula grandis, Blumen.

a. —— obliquata, J. Sow.
triangularis, Mont.
Astarte digitaria, Linn.
Cyprina Islandica ?, fragment.
rustica, J. Sow.

Tapes virgineus, Linn.
texturatus, Lam.

The next well-marked division of the Red Crag is that from which
I obtained the principal part of the fauna described in the ‘ Mono-
graph of the Crag Mollusca.’ It occupies the country lying between
the Stour and Deben, as well as the left bank of the estuary of the
Deben ; and its richest development in the yield of mollusca is on
either side of that estuary. In physical structure it is unlike that
of Walton (which is principally stratified horizontally, and due to
subaqueous deposit), and possesses for the most part that highly
oblique bedding which I now believe can have originated only in
beach-action. In this crag we have the intermingling of the greater
proportion of the Walton fauna with that northern fauna which
forms the preponderating or characteristic feature of the succeeding
horizons, to which I have hereafter to refer.

In the Sutton Crag the following species, common or not un-
frequent at Walton, have never been found by me except under the
suspected character of derivatives from the Coralline Crag— Ovula
spelta, Columbella sulcata, Nassa elegans, Natica catenoides, N. multi-
punctata, Nucula levigata, Cardium Parkinsoni, and others; while
on the other hand the following species, foreign to the Walton deposit,
occur, viz. Tritonium antiquum (dextral var.), Cardium Grenlan-
dicum, Leda lanceolata, L. imatula, Cardium angustatum, Tellina lata,
LT. obliqua, T. pretenuis, Mactra ovalis, Mya arenaria, M. truncata,
and others. The peculiarly northern forms, however, so charac-
teristic of the higher horizons, are comparatively rare, and the whole
facies of the fauna presents the appearance of that transitional state
which is intermediate between the more southern or Mediterranean
fauna of Walton and the more peculiarly British and northern aspect

544 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

afforded by the Crag of Butley, which I have now to mention. It will
be convenient for reference if I designate this as the Sutton Crag.

The district intervening between the banks of the Deben and the ~
exposure of the Red Crag around Butley is occupied by high heath-
land formed of the sands interposed between the Crag and Boulder-
clay ; and, the coast-line corresponding to it being low, we have no
recurrence of the Red Crag until we come upon that exposed by the
denudation of the Alde valley around Butley, Chillesford, and ©
Sudbourn. The Crag there, although in physical structure entirely
resembling that between the Deben and the Stour, possesses a
dissimilar fauna. In it there are, however, many of the forms
which characterize the Sutton Crag; yet they are subordinate to
those of northern aspect, which begin here to preponderate. For
instance, although Pectunculus glycimeris, which is so abundant in
both the Walton and Sutton horizons, is present, and in the lower
part of the Butley Crag not uncommon, yet it becomes subordinate

_to such forms as Tellina obliqua, T. pretenuis, and Cyprina Islandica,
which here begin greatly to prevail. In the upper portions of this
Crag, namely that upon which at Chillesford and Tunstall Heath the
Scrobicularia-crag rests, this feature is yet more marked, and the
Pectunculus becomes a rare shell, while Mya truncata, Tellina obliqua,
T. pretenuis, T. lata, Cyprina Islandica, and Mactra ovalis, which
form an enormously preponderating proportion of the Chillesford
bed (e of diagram), become especially abundant. This is the Crag
which is found at the base of the pit below Chillesford church, in
several of the pits in Butley parish, and in that one pit near Sud-
bourn church in which the Red Crag is seen resting on the Coralline.
It also occurs in a run-down pit upon Tunstall Heath.

Resting upon this Crag, in the pit under Chillesford church,
occurs the uppermost portion of the Red Crag. It is slightly oblique
at the base, but becomes horizontal in its upper beds, gradually losing
that red colour to which the Red Crag owes its name. The actual
horizon at which this Crag sets in is marked in a distinct manner
by the incoming of a shell not yet found in the lower horizon, namely
Scrobicularia piperata. This shell, although thus abruptly appearing,
occurs in profusion, and in association almost exclusively with those
forms which greatly preponderate in the Chillesford beds, namely Oy-
prina Islandica, Muctra ovalis, Tellina obliqua, T. lata, T. pretenuis,
and Mya truncata. These shells form almost the entire fauna of the
uppermost portion of the Red Crag, showing a great contrast to the
richer fauna of the older horizons. The Scrobicularia again becomes
extremely rare in the Chillesford beds. Only one other pit is known
to me in which this Crag occurs: itis on Tunstall Heath, distant 6 fur-
longs N.E. by E. from Chillesford church, marked on the Ordnance
Map “‘Sandpit.” Divided from this Crag by only about 4 or 5 feet of
brown sand, occurs the true Chillesford bed described by Mr. Prest-
wich in 1849, and industriously searched by me afterwards. The
fauna derived from this bed (e of diagram) and from the other ex-
posures of the same formation in northern Suffolk is contained in
the subjoined list :—

1866. ] ars WOOD—RED CRAG. o45
List of Shells from the Chillesford Beds.
co ao] 3
S| 82/
S)ae|as] g
Ss | S [RE| @
5 ep} &
Buccinum undatum, Linn. ......... ae) leeds: L aeislaiss x | Rare
Tritonium antiquum, Linn. ......... ae eee. ae sees Rare.
Ponpura lapillis; L272. ......-cc0cerfeseee x | *
Cerithium tricinctum?, Brocchi ...)......).cc...'eeeees *
Turritella communis, Risso ......... *
Hitorina litorea, Linn. ....:....6..00: * | « | * | x
Natica catena?, Da Costa ............ Pa De ola eae *

PSTN Fe scaioo ec vsonncheeeussfgnsed-[oenacs ee a x | N. Alderi? (Fisher.)

lansa. B70, & SOW. ccccccnscen|escecslecsas *

helicoides, Johnston ............|...00 *
Actzon tornatilis, Linn...........s0...|.....- *
MIST M A DUCCITICR ........65.00.c0ecoccledaconleaeedalessoen x | (Fisher.)
RTE TOMER cnn ciency oon neseveyea[snevge| donne koe * | (Hisher.)
SPOR LOOION GA... <n nccaceasacencensclennnee|aassme|ea eve’ * | (isher.)
Mytilus edulis, Linn, ............0+05+ Ke ed
Pecten opercularis, Linn. ............ * | x

RAUL? is sy avnwalecwodbac|eseodeakes. *
Modiola discrepans?, Monzé. ......... *
Nucula Cobboldiz, J. Sow. ......... x | * | *

SLT eae *

Leda lanceolata, J. Sow...............- SE toe A Not uncommon.
limatula (myalis) ............... * | * | * | # ;
—— semistriata, S. W00d .....0.00...|..sc0-feceeee Moke. tam Fragments.
Cardium edule, Linn...........s.....0- Se die olde oe *
BEACON IOI. oa. ainnecacseesnlencsanlaccess *
Greenlandicum, Chemn......... % | #2?
Prawagta Bemis, J. SOW, ...:...c0cs.ce.|.-soecfencens *

5 SSIS CO aie an ee se | Rae ate eat ae eee (S. P. Woodward.)
Scintilla ambigua, Nyst ............... *
uucima borealis, F772. .............065 Sle (EePa *
Cyprina Islandica, Linn. ............ x | * | * | * | Fragments.
Astarte sulcata, Da Costa ............|. Br steleen tad *

eompressa, Monts 0.2.20 lets. *
Tellina crassa, Pennant ............... *

BINGO cero isle sip wis whine gras * | * | * | * | Abundant.
—— obliqua, J. Sow..........eeeeeee. x» | * | « | x Id.

preetenuis, Leathes............... poe ke ae Id.
Mactra ovalis, J. Sow.- .......... ee % * * * Id.

SUERUMESTA De ota cdi cdaesiida trois ag [Sieendlamea eld a teas * | (Fisher.)
Scrobicularia piperata, Gmel. ...... aml On ee eee ME One specimen.
call tthe Ld ge gs AN 4 7, Sa ee = ee |
Panopza Norvegica, Speng. ......... *

Corpula sina COW sooo... cece ence lone oak x | %
liar arenmarias LGR 5. cian aneis vie veo! can eos * *
UTED CoG Mal 07: /)7, a * fs | ec ae |e a Abundant.

Besides the above, Mr. John Taylor, of Norwich, has given, from
what he terms the Upper Crag at Bramerton, Postwick, and Thorpe
(which my son regards as the Chillesford bed), Astarte borealis,
LIncina dwaricata, Scalaria Grenlandica, and Calyptrea sinensis.

In addition to this, Mr. Rose has sent me the names of the
following species from Toft Monks, from the “Lower bed;” but

546 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

as this may not improbably belong to the horizon of the Fluvio-
marine Crag itself, or at least of the sand intervening between that
Crag and the Chillesford beds, I append them separately, viz. :—

Pecten opercularis. Circe minima.

Pinna. Donax trunculus.
Nucula nucleus. Saxicava rugosa.

Leda myalis. Clavatula turricula.
Diplodonta rotundata. - Cancellaria costellifera.
Venus ovata. Scalaria Groenlandica.
Tapes perovalis (?). ; Ringicula buccinea.

The foregoing list from Toft Monks is entirely on the authority of
Mr. Rose; the others are upon my own, unless where otherwise
expressed.

With respect to the false-bedded and horizontal or water-depo-
sited Crag, which seems to occur in channels cut through the oblique
or Beach Crag of Sutton, and at the base of which only the Coprolite-
beds occur, it is difficult to bring it into a satisfactory correlation
with any of the other horizons to which I have alluded. The bed
is composed of such degraded materials, being in the upper part
almost entirely comminuted, that one cannot resist the mference
that it has been derived, in great measure, from the destruction
and redeposit of the material of the oblique Crag which surrounds
it. From this circumstance, its fauna cannot be satisfactorily arrived
at, as the greater portion may be, and probably is, derivative ;
added to which, the existence of the phosphatic nodule-band, with
its miscellaneous assemblage of fossils of various ages, marks it as
something altogether distinct from the beds of the Red Crag in
contact with it. I have myself verified the fact which has been
pointed out, that angular and apparently ice-borne chalk-flints
occur in it; and this circumstance would certainly seem to point to
its age being rather that of those upper horizons which I have
described, in which the northern forms prevail, and where ice-
transport came into action, than that of the surrounding oblique-
bedded Crag of Sutton, in which so large a proportion of the more
southern types that are peculiarly the characteristic of the Walton
Crag are intermingled: and it may be, as my son supposes, that the
lower part of this Crag is the water-deposited equivalent of the
highly-beached and oblique Crag of Butley and Chillesford, and the
upper that of the Scrobicularia-Crag. Certain it is that, unlike the
oblique Crag, which everywhere presents a rugged surface to the red
sands which overlie it, this phosphatic nodule-crag passes up into
those sands by interbedding.

EXPLANATION OF THE DIAGRAM SECTION.
By 8. V. Woop, Jun., Esq., F.G.S.

The line of section starts north from a point about 6 miles south-west of
Chelmsford, and proceeds through Chelmsford and Witham to Colchester ;
then turning east, reaches the sea near Walton Naze. It proceeds thence to
near Woodbridge, whence it turns north-east, and reaches the coast again at
Aldborough, which it follows as far as Pakefield, whence, turning north-west,
it is carried through Beccles, Rockland, Bramerton, Brundall, and Thorpe, to
Norwich. Proceeding thence in a northerly direction through Wroxham,
Coltishall, and North Walsham, it reaches the coast again at Hasborough, and

1866. ] WOOD—RED CRAG. 547

follows the coast to Weybourne, and, running thence parallel to the coast,
terminates near Wells.

a, Chalk. 0, London Clay. ¢, Coralline Crag. d, Red and Fluviomarine
Crag, divided as follows :—d', Walton Crag; d?, Sutton oblique or Beach Crag ;
d°, Butley oblique or Beach Crag ; d?+, Horizontal Crag, with phosphatic nodule-
band at the base; d*, Scrobicularia-crag, slightly oblique at the base, but hori-
zontal in the upper part; d‘+, Alternations of sand and comminuted shell
overlying phosphatic nodule-Crag (equivalent of d*); d*’, Fluviomarine Crag ;
d* and d”, Unfossiliferous sand (equivalents of d* and d'); these sands are
20 feet and more in thickness around Southwold and Aldborough, but attenuate
near the edge of the Crag in Norfolk, thinning there from 11 to 4 feet in
different sections. ¢, Chillesford shell-bed (Mya-bed of Fisher; and at Bra-
merton, Postwick, and Thorpe near Norwich, this is the Upper Crag of
J. Taylor); this bed is not constant, although the sand containing it is so: the
prevalent shells of this bed are Tellina obliqua, T. pretenuis, T. lata, Cardium
edule, Purpura crispata, Intorina litorea, Cyprina Islandica, Mactra ovalis, and,
at Chillestord, Mya truncata: the Telling prevail over all others; mammalian
remains occur in it at Chillesford, Haston Cliff, and Saxlingham; ¢’, The Chil-
lesford Clay; laminated clay interbedded with sands at the top; the base of
this clay contains in places the shells of e. jf, The Bure-valley beds: these are
fossiliferous only in places, and only where they rest on the chalk, the shells
occurring in small patches; they consist of sands with shingle-beds: the pre-
valent shells are Tellina obliqua (very common), Cyprina Islandica, and Car- .
dium edule (T. pretenuis and T. lata cease to prevail): these beds are often
considerably indented into &. g, The Lower Drift, or Lower .Glacial, divided
as follows:—g', The Weybourne sand; this thins out between Mundesley and
Bacton. East of Cromer it is generally stained,with the débris of beds dd, and
becomes in places, particularly towards Mundesley, laminated with clay bands,
in which condition it forms the laminated beds of the Rev. J. Gunn. Between
Cromer and Weybourne it (or at least the base of it) forms the Norwich Crag
of Samuel Woodward, of Sir Charles Lyell, and of the Rev. J. Gunn. ~The
prevalent shells are Tellina obliqua, Cyprina Islandica, Purpura crispata,
Cardium edule, and Tellina Balthica (solidula), which latter shell here makes
its appearance in profusion. The occurrence of this shell at any lower horizon
is doubtful; and 7f it does occur, it must be excessively rare. It is given by
S. P. Woodward from Postwick ‘top bed ;” and a specimen is in the Norwich
Museum, marked from Coltishall; but these are doubtful localities. Tellina
lata and T. pretenuis have either disappeared at the horizon of g’, or become
too rare to be readily detected. It also yields mammalian remains. g?, Tho
Cromer Boulder-Till (Boulder-clay of Sir Charles Lyell and Lower Boulder-
clay of the Rev. J. Gunn). This at one extremity passes into a white marl,
formed of redeposited chalk finely ground up. g?, The Contorted Drift. This
bed ceases to be contorted east of Mundesley, and becomes regularly and closely
stratified. Between the termination of the coast-section (at Hasborough) and
North Walsham, it passes into a tenacious green Brick-clay; approaching the
coast, near Yarmouth, it changes to a reddish sandy brick-earth, and further
south into red sand. West of Weybourne it changes into chalky loam and
sand with chalk-grains. g*, Intermediate beds of gravel occupying deeply-cut
troughs through g® and g? and underlyingh. kh, Middle Drift or Middle
Glacial: sand and gravel. This bed is chiefly fine, light, yellow, siliceous
sand; but towards London, and where present in the more central counties, is
extensively interbedded with gravels, and sometimes with thin beds of sandy
brick-earth. 7, The Upper Drift or Upper Glacial, being the widespread true
Boulder-clay, of great thickness before denudation. dd, The Forest-bed and
gravel, containing fluviatile shells and mammalian remains, being probably
the land equivalent of the beds from d' to f. This has been destroyed in part
by the waters of g!. N.B. The so-called Forest-bed at Easton Bavent is a
post-glacial and very recent peat, occupying the valley-bottoms and occurring
on the beach only in the places where the valleys open to the sea, The dotted
lines show the continuation of deposits, where their distinctive characters are
obscure, or where they are represented only by an undistinguishable mass of
sand, except in the case of the Fluviomarine Crag (d?’), which may not be
continuous, but possibly the deposit of more than one estuary.

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1866.]

590 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

The perpendicular lines in the diagram indicate the sections afforded at the
following places :—

bo

ID of w

© CO

10.

Le

12.
13.

14.
15.

16.

Li.
18.

19.

20.

. That by numerous pits south-west of Margaretting, in Essex.
. That by Margaretting railway-cutting and by pits in the Chelmer valley

above Chelmsford.

. That by the railway-cuttings and by pits between Chelmsford and Marks Tey.

N.B. h ts unavoidably represented too thin in the above localities.

. That by the cuttings near Colchester.
. That by the cuttings of the Tendring Hundred Railway, between Colchester

and Thorington.

. That by Frinton Cliff, near Walton-on-the-Naze ; 4 remains here in patches of

only a few feet in thickness, capped by a warp containing fragments of 7.

. That by Walton-on-the-Naze Cliff. The beds & here overlap the Crag and

rest on the London Clay to the south, but not at the north end of the
cliff; ¢ occurs in a few faint patches only, and the shells are too decayed
for extraction.

. That by Bawdsey Cliff.
. That by a pit immediately on the Sutton side of the Woodbridge ferry, and

by a pit a furlong south of Ferry farmhouse, Sutton. In the former pit
the beds ée’ are slipped from their place, and are marked by a clump of
trees growing on them, but in the latter are iv situ.

That by the pit at Wilford Bridge over the Deben, and by numerous pits in
Ufford adjoining. The Crag is found by digging in the Wilford-Bridge
pit. (The vertical line 10 should have been drawn only into the upper

art of d?.

That by the Coprolite workings of Sutton, Shottisham, Foxall, Newbourn,
and Brightwell.

That by the pits at Butley, near the Abbey, and near the Oyster Inn.

That by the pit behind, and by that below Chillesford church. N.B. The
Boulder-clay (z) has, by a down-throw, been slid obliquely on to é in
the former pit; but 7 and 4 may be seen in their true relation in a pit
distant one furlong N.N.W. 7 may also be seen faulted down beside d*”
and d” in a pit (marked “ Sand pit” in the Ordnance map) by the river,
9 furlongs E.S.E. of Chillesford church.

That by a pit 7 furlongs N.E. by N. of Sudbourn church.

That by several pits in Iken and in parts of Sudbourn from 2 to 3 miles
N. and N.E. of Sudbourn church. N.B. By reason of the tortuous
boundary afforded by the ridge of Coralline Crag rock to the bay in which
the Red Crag was accumulated, the Red Crag reenters the district, as a
spit, near Section 14, and does so again in small dimensions at Ald-
borough. This is not shown in the diagram.

That by the clay-pit 5 furlongs, and by the (Thorpe) crag-pit one mile
E.N.E. of Aldringham church, and by the sand-pits and railway-cutting
south of the crag-pit.

That by the country between the clay-pit and the west side of Aldringham
Green.

That by Dunwich Cliffs. N.B. g* is represented in these cliffs by a dark-
orange sand which comes up in the southern part of the cliff-section ; / is
very thick here (about 50 feet). 7 occurs for a few yards only, and imme-
diately north of the ruins. There is also a deep bed of post-glacial gravel
under the ruins, and a later post-glacial yellow loam, as well as a black
warp over all.

That by Southwold Cliff. The cliff is too obscure to show whether the sand
forming much of it is , or is post-glacial; but at the north end (at the
kiln) z, together with thick post-glacial beds capping it, and containing
freshwater shells, has been thrown nearly into the vertical.

That by the clay-pit 2 furlongs east, and the crag-pit 4 furlongs north-east,
of Henham-Park farm; and by various sand-pits along the Blyth valley.
N.B. i may be seen faulted down beside d” and d” in a pit by the farm-
house 3 furlongs H.S.E. of Bulchamp Workhouse, and the same distance
N.N.E. of the Bulchamp crag-pit. A pit of oblique-bedded rounded
pebbles occurs close to the 101 milestone, E. of Henham Hall, and another

1866}. = = =~=——sC Woop — RED CRAG. 551

2]

amie

22,

25.
26.

3l.
32.

6 furlongs N.N.W. of it, which are worthy of special visit; the latter
shows continuous oblique bedding in a vertical section of 25 feet. They
seem to be beaches of the age of f, but may be of that of d?. In the clay-
pit a piece of the upper bed of e’ has been transported, dropped again,
and interbedded with f.

That by Easton Bavent Cliffs.

That by Covehithe Cliff. N.B. There isa bed of loam, sometimes contorted,
resting on a denuded surface of e’ at the north end of Easton and south
end of Covehithe Cliff; but it seems to be post-glacial and to have no
connexion with g*. There is also a post-glacial gravel-capping to the
cliff, and a more recent sand in the valley-depression. Similar sections
to 21 and 22 occur in several brick-fields between Wangford and
Frostenden.

. That by Pakefield Cliff. g* comes up at the base of the cliff, but is better

exposed at Corton Cliff, 6 miles further north (and out of the line of
section), where it is at one part contorted, with gravels in the con-
tortions; / is here thinner, varying from 25 to 35 feet.

. That by the Brick-field at Toft Monks, near Beccles, 5 furlongs N.N.W. of

the 110th railway mile-post.. N.B. The gravels capping ¢ in the section
are not the bed f, but post-glacial. Post-glacial gravels also occur in a
pit immediately north of the kiln, sharply faulted down beside 2. By
ascending from the Brick-field for a furlong, the beds up to and in-
eluding ¢ are passed over.

That by the Brick-field at Ingate, Beccles.

That by numerous pits near Rockland Staith, and in Surlingham (6 miles
east of Norwich). In one pit at Rockland Staith, g* is faulted down
beside f. Ina pit at Surlingham Wood the upper beds of e' are late-
rally squeezed up, the lower remaining horizontal. The upper beds of e'
are also much eroded by the shingle-beds of f/ The sections in & and t
are on the top of the hill. .

. That by the Bramerton Crag-pit.
. That by the hill descending to the Crag-pit.
. That by the pits behind Brundall Station, and beside the railway 4 fur-

longs west of that Station.

. That by the Crag-pit at Thorpe, near Norwich. N.B. The Postwick-Grove

Crag-pit adjoining includes from d?’ to e only. In the section in the pit
east of Postwick Church d?’, d?', and d*' seem absent, and e to rest on the
chalk, showing the rapid approach of the edge of the deposit. The same
is the case at Saxlingham, which is out of the line of section. At the pits
on Smockmill Common, Saxlingham, the shells are in a friable condition,
and e is sand; but at the pits 3 furlongs W.N.W. and 5 furlongs 8.W.
by W. respectively from the Baptist Meeting-house, Saxlingham, e is in
the condition of gravel with mammalian remains, e at these places
resting on the Chalk. e’ caps e in all the pits at Saxlingham, although
its development is feeble.

That by the Brick-earth-pit, 2 furlongs N.N.W. of the Thorpe Crag-pit, and
the Brick-field one furlong further N.N.W.

That by numerous chalk-quarries and brick-pits near Bishop’s Bridge,
Norwich, and on the Catton side of Mousehold Heath. N.B. The Heath
itself is capped by a very deep bed of post-glacial gravel.

. That by the Brick-fields at Plumstead Street, 6 miles north-east of Norwich.
. That by the Brick-pits } mile north of Wroxham Bridge, by Horstead Marl-

staith, and by the Lime- and Brick-kiln immediately north of Coltishall
village. N.B. It is only in this neighbourhood that the bed / has yielded
fossils.

. That by the heath-country between Westwick and North Walsham.
. That by two deep pits 6 furlongs south-east of North Walsham.
. That by the Brick-pits and Marl]-pits in the valley of North Walsham. 4g?

- occurs here in the form of very chalky marl coming out in the bottom of
the valley.

. That by Edingthorpe Heath. —

VOL. XXII.—PART I, 2p

552 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

39. That by the Brick-pit on Edingthorpe Heath, 6 furlongs E. by N. of Austin
Bridge; a sharp anticlinal a few yards wide brings g* to the surface here.

40. That by Hasborough Cliff. The upper part of g* here consists of finely strati-
fied silt, which in places is deeply denuded, the base of h occupying the
denuded depressions, in some cf which partial bands of brick-earth occur,
which form, I believe, the Upper Boulder-clay of Mr. Gunn at this place.

41. That by the Cliff north-west of Bacton, east of Field Barn.

42. That by the Cliffs further west, and N.N.E. of Field Barn.

43. That by the Cliff near Mundesley. g*, which has hitherto been regularly
stratified, begins to become contorted. N.B. There is a post-glacial bed
in the valley at Mundesley.

44, That by the Cliff near Beacon Hill, Trimmingham. 4g’ here cuts in places
through g? into g?; the dimensions of the diagram do not permit of
this being represented. N.B. g', which has hitherto been black with the
débris of dd, becomes yellow sand and ceases to be laminated.

45. That by Felbrigg Heath.

46. That by the Cliff near Cromer. g*is here and in Nos. 47 and 48 divided
from / by an indurated grayel-pan. N.B. Between 44 and 46, 9’ again be-
comes stained with the débris of dd and partially laminated.

47. That by the Cliff near Sherringham. |

48. That by the Cliff near Weybourne. N.B. Midway between 47 and 48,
g° begins to lose its contortions, and to become stratified again; g? and
g° also become difficult of distinction, and together to assume the con-
dition of chalky loam.

49. That by Weybourne and Kelling Heaths.

50. That by Salthouse Heath.

51. That by various pits in the valley of the Glaven. g? and g° are here repre-
sented. only by chalky loam, or marl, with occasional beds of chalky sand.

52. That by Saxlingham Heath (6 miles from Weybourne).

The section as it stands in No. 52 is continued west to Wells, except that / is
almost wholly denuded, g? and g? occupying the surface of the country through
Field Dalling, Binham Abbey, and Wigton. In a pit 4 furlongs east of Copy’s
Green, Wigton, a sand comes up beneath g? and g® (which are represented by a
sandy chalky loam). This may be the recurrence of g' at this part.

By the Railway-cutting east of Wells Town a very fine section is afforded of
g? and g*, in the form of a chalky loam resting on the chalk and partially
underlain by boulder-gravel. South and south-west of Wells, 2 comes on again
in thickness at Holkham Triumphal Arch and near Fakenham.

By the term “post-glacial” is meant beds that have been deposited sub-
sequently to the great denudation which ensued upon the close of the formation
of 7. None of these appear in the Diagram, which represents the state of things
at the commencement of the formation of 7.

It will be seen by the above that the Chillesford beds, e and e’, and the sand-
and pebble-beds, f, which, by reason of their strict conformability to the base of 2
over the crag area, were tréated in the “‘ Remarks in explanation of the Map of
the Upper Tertiaries of the Counties of Norfolk, Suffolk, Essex, Middlesex, Hert-
ford, Cambridge, Huntingdon, and Bedford, with parts of those of Buckingham
and Lincoln, and accompanying sections,’ as belonging to the lower part of ,
are no longer so regarded. Their true position in the sequence of deposits has
been arrived at by tracing the thick Contorted Drift of the coast, through a
series of unequivocal sections, into the comparatively thin bed of brick-earth
which overlies the sand and pebble-beds, f, near Norwich.

This modifies the interpretation put in the ‘“ Remarks” upon Nos. 9, 10, 14,
24, and 25 of the sections accompanying them,—Zé in that part of section 9,
which is near Norwich, comprising the beds e, e’, f, and g’ of the above Diagram ;
and in the western part of .section 10 the beds f and g*, in addition to the
Middle Drift 4; while in section 14 it includes at Sudbourn, Aldborough, Thorpe,
Easton, and Covehithe the beds ¢, e', and f; and at Kessingland and Corton the
beds g? and ’. In section 24,4. represents d%' d¥, e, and part of ¢, and in
section 25 the beds from the base of f to the middle of .

1866. | FISHER—WARP. 553

2. Note on Surrosep Rematns of the Crag on the Nortu Downs near
Forxsrstone. By H. W. Bristow, Esq., F.R.S., F.G.S.

On my return to London, after an excursion made in May 1857,
in company with Sir Charles Lyell, Professor Ramsay, and Messrs.
Prestwich and Godwin-Austen, to the district of Kent, from which
fossils had been got which were thought to be of the age of the Crag,
I made a memorandum on the subject, of which the following is a
copy :—

‘‘ With regard to the sands, &c., seen at Paddlesworth and else-
where, accompanied by thin bands of iron-grit, I have seen nothing
from which it would be at all reasonable to infer that the beds in
question were any other than those of the Lower Tertiary (that is,
of the Woolwich and Reading series), occurring in their proper posi-
tion on the denuded surface of the Chalk.

“< Beds like the Paddlesworth ferruginous sands occur in the Hamp-
shire Basin, where a part of the Woolwich and Reading series is
represented by ferruginous clayey sands, with masses of ferruginous
grit, &e*. Another strong resemblance is also borne by these last
beds to those of Paddlesworth in the red colour of the sands, as may
be observed more particularly at Whiteparish, in Wiltshire, where it
would seem that when the mottled clays are replaced by sands the
colouring matter is often persistent although the mineral character
of the rock varies. With regard to the greater development of ferru-
ginous grit at Paddlesworth, that alone is not enough to afford re-
liable evidence one way or the other, and in either case it might be
a mere local condition over the particular area in question, iron
being more or less diffused throughout the lower London Tertiary
beds—in some cases (as in that of the basement bed of the London
Clay over a small area in Dorsetshire) to the extent of furnishing a
very rich bed of iron-ore, which, under favourable circumstances,
would prove highly valuable for smelting-purposes.

“‘ If these Kentish beds can be proved to belong to any other mem-
ber of the Tertiary series, it is only to be done by a careful exami-
nation of the evidence given by the fossils. There ought to be little
difficulty in this, from the very great interval between the two sets
of strata, and from the fact that about 50 per cent. of recent forms
ought to be found in beds of the age of the Lower Crag.”

P.S.—From an examination of the fossils shown to him at that
time, Mr. W. H. Baily believed them to be of London-Clay age.

3. On the Warr (of Mr. Trimmer)—zts AcE and probable Con-
NEXION with the Last GroxoaicaL Events. By the Rev. O. FisuEr,
M.A., F.G.S.

[ Abridged. ]
I am not aware that any geologist since the late Mr. Trimmer has

* The ferruginous bands at Paddlesworth are not seen to be fossiliferous ; and
the fossiliferous ironstone from the pot-holes at Lenham is not seen in place,
and may therefore belong to any period.

2P2

504 PROCEEDINGS OF THE GEOLOGICAL SocIETY. [June 20;

devoted a paper to the elucidation of the subject of what he has
called the “ warp ”’ or the “ warp of the drift”’*. In his paper “On
the Soils of Kent” he lamented the slight attention that had up to
that time been paid to “the period which intervened between the
desiccation of the bed of the glacial sea and the commencement of
the historic era of geology.” Had Mr. Trimmer lived until the pre-
sent day, he would have seen the earlier part of that period receive
at least its due share of attention. The closing portion of it, which
saw the formation of that warp or subsoil on which the fertility of
our fields chiefly depends, has not, so far as I know, received any
particular attention since Mr. Trimmer’s valuable labours were pre-
maturely terminated. |

My attention has for some time past been attracted to this
subject, and in my paper on the Brick-pit at Lexdent I hinted
at its importance as containing records of the latest geological
changes.

Mr. Trimmer appears not to have arrived at any satisfactory conclu-
sion as to the causes"which have produced the warp. He says, “‘ The
majority of soils and subsoils in the British Isles are composed only
in part of the débris of the rocks on which they rest, and in part of
materials transported from various distances by forces of consider-
able intensity, differing from ordinary atmospheric action, which
were in operation at the close of the glacial period. I have called
these results the warp of the drift or the erratic warp”t. But he
leaves us in ignorance as to the nature of these forces, farther than
that, in his “ Geology of Norfolk” (Journ. Agric. Soe. vol. vii. p. 465),
he says that “it appears to have been a deposit from turbid waters
returning to a state of tranquillity.” Nevertheless, in his paper “On
the Soils of Kent,” first referred to, he speaks of the great variability
of soil within a few acres. This is a well known fact, and appears
incompatible with the explanation of the warp being thrown down
from a flood of turbid water, which must have produced very equable
soils over moderate areas. .

In stating that the warp differs more or less from the subsoil on
which it rests, Mr. Trimmer adds that “on sands it contains a
greater mixture of argillaceous matter, producing a sandy loam of
different degrees of adhesiveness ; on clay it contains an admixture of
sand, producing a clay loam, or, at any rate, clays less adhesive than
than those of the subsoils.”

These remarks are undoubtedly just. The warp is influenced in
its character by the stratum on which it rests, but at the same time
often contains ingredients which cannot have been derived from it.

Whence, then, Fhaveniiese ingredients come ?

‘It is well known that the surface of the subjacent stratum, wher
ever it is of a soft nature, such as clay, sand, gravel, or chalk, is
worn into furrows and hollows, sometimes into pits and pipes. The
sections I have chiefly had an opportunity of studying for the pur-
pose of this paper have been in clay, sand, and gravel, which have,

* Quart. Journ. Geol. Soc. vol. vil. p. 31.
t Ibid. vol. xix. p. 396. { Loe. cit. .p. 32.

1866.] / FISHER—WARP. 555

for my present purpose, an advantage over calcareous strata, in that
they are not soluble by water, and the phenomena therefore are less
complicated. As far as my observations extend, I have found that
cylindrical pits and pipes are generally confined to soluble beds, and
that the normal form of the cavities in clays, sands, and sravels i is
that of troughs or furrows*. They are usually filled with materials
derived from some neighbouring higher ground, and consequently
generally differing from the subjacent stratum at that spot; and it is
by the admixture of the contents of the furrows with the material of
the subjacent stratum that the warp, which is derived from the two
conjointly, comes to contain materials mixed in a different propor-
tion from that in the subjacent bed.

These furrows must be important indications of the mode of de-.
nudation of those surfaces where they occur; nevertheless, being
simply the tool-mark of the Jast agent which has moulded the sur-
face, if we could determine from them what that was, we need not
exclude other and different ones which may have preceded it.

For the sake of a name I shall call the materials which fill these
furrows the “ trail.” And I will now give a few examples of them
in diagram. .

Fig. 1.—Section of a a which crosses the Tendring Hundred
Railway, near Great Bentley Church, Essex.

Railway.

It is 7 feet deep, full of grey sandy and gravelly clay (4), eroded in brown sands
(c). The warp (a) covers it. There is a layer of pebbles at the bottom of
the furrow, and roots have penetrated throughout it. The gravel is more

- angular than that of the glacial drift from which it has been derived, many of
_ the rounded pebbles having been broken up into angular fragments.

At the gravel-pit, Ballast Quay Farm, near Wivenhoe, Essex, two
masses of trail have been left, being too clayey for use. They are
parallel to each other; one of them is fifty yards long, the other not
much less. Erosion has gone on beneath them, which is shown by
the pebbles of the warp, and also of the trail, lying in festoons.
They are inclined at a small angle to the surface- drainage. They
occur in sandy glacial gravel.

* For examples of these troughs, see figs. 1 and 5. London clay dug for
ballast at Bentley Tey, near Great Bentley, to the depth of 5 feet, exposed a
section of a furrow ten yards long and a yard wide, running in the direction of
the drainage of the surface.

006 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

And first, as I have already observed, the trail is derived from
some not very distant point of higher ground.

Secondly, where the trail contains pebbles it will be noticed that
their axes, more frequently than not, deviate from the horizontal
position.

Thirdly, the trail sometimes contains portions of incoherent beds,
which nevertheless are not scattered and disseminated as would be

Fig. 2.—Section of Trail in a Pit east of Chillesford Church, Suffolk.

a. Warp defined by an intermittent layer of pebbles of chalk and small flints.
6, Trail from Boulder-clay with chalk and oolitic pebbles and fossils,

ce. A layer of drift from the Chillesford Clay.

b'. Drift from the Boulder-clay, a repetition of 6.

d. Chillesford Clay.

Fig. 3.—Section of Trail at Calne Railway-st

ae

a. Warp. 6. Trail of red sandy gravel. ce. Coral rag.
Fig. 4.—Section of Trail at Woking, Surrey.

———

b. Trail, with axes of peb-
bles mostly vertical.

ec. Sandy clay horizontally
stratified. The locality
is nearly level.

the case if they had been water-drifted. I have noticed this fact, espe-
cially, in some Crag-pits in Suffolk. For instance, in the large Coral-
line Crag-pit near Aldborough, Mr. 8. V. Wood, jun., has mentioned
patches of what he supposes to be Red Crag, and also phosphatic
nodules, overlying the Coralline. Both of these occur in the trail.
The so-called Red Crag probably consists of a portion of the Mya-
truncata bed, which would occur in ordinary sequence a furlong or

1866. ] FISHER—WARP. 507

so up the hill. The drifted fragment is much distorted, but never-
theless not scattered. There are similar patches of this bed in the
trail in an old Crag-pit on the Saxmundham road, about a mile and a
half from Aldborough.

A similar case was seen by Mr. Boyd Dawkins and myself at
Walton-on-the-Naze, where an angular lump of London Clay, about
eighteen inches in diameter, was entirely enveloped in a mass of
gravelly trail.

Fig. 5.—Section across a furrow of Trail covered by Warp, left
standing after the removal of the surrounding gravel for ballast,
Wivenhoe, Essex.

a. Warp.
6. Trail.

The position of the pebbles in the trail, and still more so the con-
torted but unscattered condition of incoherent material, show that
_the trail has been transported in a plastic state (as mud) moving by
its own gravity, or else pressed onwards by some other agent.

Fig. 6.—Sectron of Trail near Villa Farm, Tendring Hundred
Railway.

a. Warp.

b. Trail of sandy gravel.

e. London clay.

d. Weathered surface of
London clay, full of
Slickensides.

I can cite instances which prove that considerable force has been
involved in this process. In a railway-cutting near Wivenhoe,
in Essex, I found at the side of a valley one of these furrows in
London clay, about 13 feet deep, filled with such sand and gravel as
caps the tableland around. The clay, for the thickness of 4 or 5
inches, was kneaded into a plastic state, laminated, and full through-
out of polished surfaces of slickensides, showing that the trail which
filled the furrow had been pushed forwards under great pressure,

558 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

and had carried forward with it the surface on which it rested. A
few pebbles, which had become engaged in the clay, had received a
considerable amount of polish. The weathering extended about as
far as the clay had been moved. A specimen of this clay is depo-
sited in the Society’s Museum. Similar instances were seen by Mr.
Boyd Dawkins and myself at Walton-on-the-Naze, and by Professor
Liveing and myself at Aldborough.

It is very desirable that the trail should diligently be searched for
organic remains. As yet I have never seen any vestiges of such,
either animal. or vegetable, within it. It will constantly be found
filled with roots; but that is owing to its inviting their presence by
the subterranean drainage caused by the usual clayey lining of the
bottom of the furrows.

As far as I have had opportunities of examining the furrows, I
have noticed that they are largest and most numerous in the neigh-
bourhood of valleys, and are either parallel or inclined at a small
angle to them. If, as I believe, they are connected with the pheno-
mena of denudation, this is what we should expect.

If there ever was formerly a universal spread of trail over the
general surface of the land, it has now disappeared, and the only
remains of it are to be found in the furrows, which he deeper than
the latest general denudation has extended.

There can be no doubt that these furrows, with the trail which
they contain, are older than the warp, and that their contents have
contributed to form the warp or general subsoil; and thus we see the
reason why the surface-soil sometimes varies so remarkably over
limited areas; for these patches of trail are not universal, and where
they occur they influence the composition of the soil to considerable
but not to great distances.

There can, I think, be not much doubt that there was a time
when our country was comparatively, if not entirely, bare of the pre-
sent covering of vegetation; for the denudation which formed these
furrows can hardly be supposed consistent with a clothing of turf or
forest. When the more severe climatal conditions, whatever those
may have been, which conduced to the denudation had passed away,
the country would become gradually covered with vegetation, and
the work of rain and rivers and frost, under their more ordinary
conditions, would commence to modify the form and state of the
surface.

Let us now consider the final preparation of the warp. Conceive
the face of the country, as the denuding forces left it, consisting of
the bare rock, thinly covered in places by the trail of material left be-
hind by that agency, and in places occupied by furrows, or shallow
hollows, filled with similar stuff. This is the foreign material to be —
incorporated with the subjacent rock to form the warp.

Atmospheric causes have operated from that distant day to the
present in bringing about the result. Rain and, during drought,
winds have tended to spread the finer materials of the surface.
Frost has affected the envelope as far as it could penctrate, mixing
the natural rock with the adventitious matters. After vegetation

1866. ] FISHER—WARP. 509

had commenced, roots have played: an important part in the work,
and the earthworm, as Darwin first pointed out *, has contributed a
by no means inconsiderable share to the general result.

_ Of these agents I will touch only upon the work of frost and rain.

And first of frost. Suppose a mass of loam containing a pebble to be
frozen, what takes place? The loam, by virtue of the water which it
contains, expands, and this expansion necessarily takes place entirely
upwards. The pebble does not expand. The consequence must be
that some of the loam, which surrounded the pebble laterally, will be
pressed over its upper surface. When the thaw occurs the soil sinks
again, and, there being now more material above the pebble than be-
fore, it is forced to imbed itself at a lower level. There is another
action which conduces to the same result. The frost enlarges in
every direction the hole in which the pebble lies. As soon as the
ice melts, the pebble sinks to the bottom of the hole, by this means
gaining a depression equal to the thickness of the coating of ice
which surrounded it. The subsequent rain and the subsidence of the
soil fill up the vacuity.

It is evident that from this cause the larger stones will descend
faster, because their relative displacement in the general loam will
be in proportion to their linear dimensions ; and the materials of the
warp will be arranged vertically according to the relative magni-
tude of the constituents, to whatever depth the frost may penetrate :
and we may expect to find a layer of stones in its lower part, as in
fact we do.

This action will, however, be modified by the effects of rain. For
that, on the other hand, carries down the finer particles of the soil
through the interstices among the coarser materials, and fills the
spaces which the frost opens; and the examination of the warp be-
neath a lens reveals this arrangement of the finest clay enveloping the
sandy particles. Pebbles taken out of the warp are also covered
with a fine polished coating of clay. Hence any layer of clay,
however thin, originally on the surface will be distributed equably
throughout the whole depth of the warp.

The erect position, already noticed,
of the included pebbles, is in many cases
common to the warp as well as to the
trail. This effect is probably not always
produced in the same way. The fol-
lowing appear to be some of the possible
causes of the phenomenon.

It is well known that a Hee or
other heavy lamina, will sink through
water with its plane horizontal. In the
same manner a pebble of an elongated
elliptical form would sink through water
with its axis horizontal. But if it sank
through mud the friction would play a
| ‘more important part than the resistance,
_* Transactions Geol. Soc. 2nd ser. vol. v. p. 505.

Fig. 7.—Diagram illustra-
ting the motion of a pebble
in a plastic medium.

560 PROCEEDINGS OF THE GEOLOGICAL SocIETY. [June 20,

especially if its motion were slow; and the effect of friction would be
to place the pebble on end. It will be easily seen in the figure that
the friction throughout the portion a will tend to place the axis
horizontal, while that throughout b will tend to place it vertical. It
is evident that the latter will preponderate.

I doubt, however, whether in nature we have cases of pebbles
which have been arrested while descending by their own gravity.
The action of frost, as indicated already, scems to be a more probable
cause of their descent; and their verticality may be thus accounted
for. The upward motion of the matrix, while expanding under the
inflnence of frost, will be, relatively to the pebble, gradually increa-
sing from its lowest pomt upwards. The friction will therefore be
greater towards the upper end of the pebble, and the effect will be
similar to that just described, but more considerable.

It will be observed that the pebbles near the sides of a furrow of
trail are more generally vertical than those in its more central parts.
This has arisen from the dragging of the materials from above down-
wards against the wall of the cavity, while it was being widened
and deepened. Ifa line be drawn through the centre of the pebble
parallel to the section of the side of the cavity, the motion of
the particles of the matrix between this line and the wall will, from
the retarding effect of friction against the wall, be less than on the
further side. Now, since the pebble tends to partake in the motion
of the enveloping matrix, it is clear that the effect produced will be
a tendency to roll it over, in the same direction that a pebble would
roll down the wall of the furrow. This tendency to roll, however, will
be resisted by the imperfect mobility of the particles of the matrix
inter se; and the resistance will be the greater the more the figure
of the pebble deviates from sphericity. Itseems, then, that when the
pebble has assumed a position in which the moment of the rolling
force is so far reduced by its position as to be counterbalanced by
this resistance, it will remain permanently so, and move forward
without further rolling. The position in question will be one in
which the longer axis is approximately parallel to the wall of the
cavity. And hence the pebbles at the sides will be more or less
nearly vertical.

Though I cannot give any measurements, I may observe that the
effects of frost seem to have extended at the time the warp was
formed much deeper than they do at present.

Mr. Trimmer has noticed, in his paper “ On the Soils of Norfolk ”
(Journ. Royal Agricultural Society, vol, vu. pt. 2), that, as a rule,
the warp is thicker upon the tablelands, thinner on the flanks of
hills, and, again, thicker in the bottoms of valleys. In short, there
has. been a slow drifting action from the higher to the lower
grounds; and it will accordingly be observed that the warp on the
sides of hills and at their feet tallies less with the fundamental rock,
but consists chiefly of the materials brought from the higher grounds.
How, then, does this drifting take place? Unless I am mistaken, it
is partly subterranean, Every one must have noticed the singularly
eroded line of junction often existing between the warp and the

13866. ] FISHER — WARP. | 561

subsoil, This I believe to be the sections of channels of drainage,
and that the drainage carries forward some material with it. Some
such action as this may account for the flat-topped elevations, like
the tenons in the framework of a dissected puzzle, which often occur
in or near the line of junction of the warp with the subsoil, espe-
cially (if I mistake not) where the latter contains calcareous matter
and has suffered partial solution. The erosion at the bottom of two
contiguous subterranean channels would leave an elevated ridge be-
tween them, and the superincumbent soil sinking in a general mass
would then flatten the crest of the ridge. By a continuance of such
a process, with slightly shifting directions in the drainage, those
complicated foldings would be formed the cause of which, at first
sight, seems so incomprehensible.

Fig. 8.—Section of a Pit in Victoria Road, Cambridge.

= a, Warp.
. 86. White sandy brick-earth.

e. Yellowish sandy earth.
d. Fine sandy gravel.
_. @ Yellowish brick-earth.
== f. Fine gravel, more contorted than the
— layers above and below.

g. Sand.
The sands contain Bythinia, &c.

Contortions of the kind alluded to, when occurring in gravel-beds,
are sometimes explained by the action of floating ice; but that cause
can only have operated under water. These contortions have in some
way or another resulted from subaérial causes; and though I see
difficulties, I think this explanation may be the right one.

In the instances from the Cambridge gravel-pits the percolation
and consequent erosion seem to have taken place in the layer be-
neath the ductile clay, which is folded into such remarkable forms.
Had it been on its upper surface, the layer must have been cut through.
It must be recollected that slight inequalities slowly formed in the sur-
face of the ground by such subsidences would be continually levelled
by the action of rain, herbage, and worms. 3

The next question which I propose to enter upon relates to the
age of the warp. The causes to which I have attributed its forma-

062 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

tion—frost and rain, wind, earthworms, and the growth of herbage—
are causes in operation at the present day; and therefore it might be
expected that the warp is the latest geological formation. Yet I
believe that conclusion would be incorrect.

It is evident that it has been formed for a long period, because the
layer of pebbles usually seen at its base will be frequently found to
have descended to the depth of a foot or more over the mouth of any
subjacent pipe which may happen to have been formed in a calcareous
rock. In a similar manner channels of slight subterranean drainage
will be found to deflect the layer. These effects must have taken some
time. But a more definite measure of its age was first noticed by
Mr. Trimmer in his paper “ On the Soils of Kent”*. He there
states that he had found “in the neighbourhood of Faversham, be-
low the level of high-water mark, lacustrine and fluviatile deposits
covered by non-fossiliferous deposits analogous to that of the erratic
warp of Norfolk.” Ihave noticed myself the passage of the warp
below the level of high-water mark in the estuary of the Colne.
About two miles below Colchester the outline of the rising ground,
marked by the unbroken continuation of the warp, passes beneath
the silt of the estuary. The surface of the silt, now reclaimed for

_ Fig. 9.—Section in a ditch on Tendring Hundred Railway,
| near Colchester.

* Low-water mark.
a, Estuarine mud of the present marsh. d. Probably London Clay.
b. “ Serobicularia”-clay. e. Gravel.
c. Warp. jf. Sandy gravel.
? The line of section on the south side does not meet the upland again, but after
crossing some marshy ground, runs into the estuary of the Colne.
Specimens from this section are deposited in the Society's Museum.

meadowland, must be about 6 feet below high-water mark. The
section was seen in a ditch by the side of the Tendring Hundred
Railway.

Another instance of the same kind in the same neighbourhood
was disclosed in the sinking of the cylinders on which the rails are

* Quart. Journ. Geol. Soc. vol. vii. p. 36.

1866.] ° FISHER— WARP. 563

carried across Alresford Creek. The first cylinder was sunk in the
marsh, the second at the edge of the tideway. The sections given
to me were :—

First Cylinder.

ft. in.
etuarme: mud. 4 0.4 .5J5e eae Me haem vetted 340
Black gravelly mud with shells............ On 46
“Yellow virgim soil,” 7. ¢. “ warp”... es 8s 3 0

Second Cylinder.
Bice Mara LAPS ATTN: Liss oh es igen tapas eoacees’ Win) aBitoys wie dem S..0
Black gravelly mud with shells............ OeNG
‘«¢ Yellow virgin soil,” 7. ¢. “ warp” ........ 30
‘«‘ Bluish-yellow clay,” probably Sees 6 0
Morar. CI wy a ce jaitvcetap site mysteysiec tie as

T examined the materials thrown out of these cylinders, and they
agreed perfectly with the descriptions given to me by the foreman of
the works. The warp was met with as far as the fourth cylinder—that
is, about 200 yards from the edge of the marsh. These facts prove
that the warp was formed before the last depression of the land ; for
the tide rises 10 or 11 feet above its surface. It may have extended
to a greater depth below high water than this ; for itis quite possible
that the reason of its not occurring in the middle of the tideway may
be, that it has been denuded.

I met with another proof of the antiquity of the warp, of a differ-
ent kind, but of a similar significance, on the same line of railway.

Fig. 11.—Section showing Warp cut off by erosion of a stream.

a SS Stream.

1
1
1
1
'
1
1
1

a. Warp. 6. Recent silt.

Just west of Great Bentley, where on the map stands the letter
«“s” in the word ‘ millions,” the railway crosses a valley. The
small stream which it contains has deepened the original valley by
about 12 feet, leaving a bank on the western side. A section of this
bank was visible in a freshly cut ditch on the north side of the rail-
way ; and it was noticeable that the warp was cut off at that point.
The soil of the recent flat bottom was a silt without any true warp
upon it. 3

I believe it will turn out that the true warp, with its line of
pebbles at its base, does not extend over alluvial flats*, but (unless
it happens to have been denuded) passes beneath the recent
deposits. In short, it accompanies the original surfaces of denu-
dation.

* No true warp was seen where the culvert was put in between Alresford and
Frating.

564 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

The surface of the high-level gravels, and of the brick-earth which
often covers them, appears to have been affected by the same fur-
rowing action which has operated upon the surfaces of older beds.
They are also enveloped by the true warp, which seems to have been
formed chiefly by severe winter frosts, and by other stibaérial causes,
before the last depression of the land ; for, as I have shown, the warp
is covered by the alluvial deposits. In the valley of the Stour, about
Sudbury, in Suffolk, the valley-gravels are to be seen furrowed by
trail from the higher grounds. The flints from the Boulder-clay in
the trail are there coarser than those in the gravel which contains
the furrows. An excellent section of the trail is also to be seen in
the Ilford Brick-pits.

We have, then, data for fixing the period of the formation of the
warp over the surface left, in all probability, in a bare condition by
a preceding general denudation. It was subsequent to the period
when the Hlephas primigenius lived in company with L. antiquus, and
when chipped implements were used; for the gravels which con-
tain those associated relics have been affected by the denudation
which preceded the formation of the warp. But it was previous
to the growth of the newest submarine forests, which occupied the
surface before the last depression of the land. It appears to have
been the period which, before the glaciers of Scotland finally disap-
peared, left the moraines described by Mr. Jamieson as having been
formed anteriorly to the deposition of the Carse clay*; for there seems
little doubt that that clay is the equivalent of the marine silt with
Scrobicularice which covers our English submarine forests, and that
the elevation which Mr. Jamieson tells us must have been so general
over a large part of the western seabord of Europet was followed
by a depression, if not quite so general, at least very extensive.

Upon reviewing the changes which have been indicated by the
phenomena discussed in the present paper, we have disclosed,
in the first instance, a condition of the surface when the general
features of the landscape were the same as at present, during which
the great mammalian fauna flourished contemporaneously with the
fabricators of the chipped flints.

We have, subsequently, though perhaps not in immediate
sequence, a period of extensive denudation, indicated by the furrows
filled with materials from the higher grounds, which have travelled
in a plastic state, and which I have called “trail.” This denuda-
tion brought the surface almost exactly to its present form. The
period of the formation of the warp succeeded, in which the winter
frosts seem to have been more severe than at the present time.

It was either during this period, or shortly afterwards, that the
submarine forests flourished. A submergence of moderate amount,
measured by a few tens of feet, next followed, and the Scrobieu-
laria-mud_was deposited over the lowest forest-grounds. The sea |
was then depressed again, and the recent period commenced.

The changes of form in the present surface which have taken
place since that time may, I believe, be easily recognized, since they

* Quart. Journ. Geol. Soe. vol. xxi. p. 173. t Ibid. p. 180.

1866. | SALTER—FAULTS IN DRIFT. 565

usually interrupt the more general contour of the surface. One of
these has been noticed, in the case where the warp has been cut off
by a stream.

When this paper was read before the Society, certain speculations
were entered into, in which it was attempted to correlate the above’
sequence of events with those indicated by Mr. Croll.as flowing from
his theory of climatal changes. It has been thought, however, that
these questions had better be reserved for future discussion, and that
the paper should appear in the present abbreviated form.

4, On Fautrs in the Drirt-eRravet at Hircuin, Herts,
By J. W. Sarter, Esq., F.G.8., A.L.S.

Ar Hitchin there is an admirable section laid open by the deep cliff-
cutting of the Great Northern Railway, which exhibits faults affecting
both chalk and an old gravel which, thanks to the investigations of
Mr. Seeley (in Cambridgeshire) and the independent research of
Mr. Thomas M*Kenny Hughes (nearer Hertford), I am enabled to
refer to the Boulder-clay period.

There is no ambiguity in this section. The chalk rises from
the railway-level in bold cliffs, 60 or 70 feet high, capped here
by chalk-drift, and there by fine, yellowish, stratified gravel—the
latter in certain spots, e.g. the lime-kilns, coming down almost to
the level of the road, and again rising up to near the top of the cliff.
The beds of chalk undulate a good deal; and the older gravel follows
its curves into curious depressed spaces, both north and south of the
station. These depressions are, as the section will show, due not to
erosion, but to faults*.

The upper gravel, which fills pipes in the chalk, and everywhere
caps both chalk and drift, is much more varied in its composition
than the lower and older gravel ; often it is a chalk-rubble, especially
along the higher ground, but interstratified with gravelly loam, full of
broken and worn chalk-flint. More commonly it is a darker-coloured,
yellow, gravelly clay or loam ; and in this latter condition it may be
seen in the large deserted gravel-pit just south of the bridge for the
high road from Hitchin, south of the station. Close to this bridge is a
conspicuous fault in the chalk, which runs across the railway, but is
most easily seen on the east side. It runs 30° E. of N.

Following this southwards, past the opening of the gravel-pit, we
again find the chalk in a low cliff-cutting, with numerous vertical
fissures, and capped by a conglomerate of rounded flint-pebbles, chalk-

* The faults in Boulder-clay, seen in the Ely section, and described by Mr.
Harry Seeley (Geol. Mag. vol. ii. No. 18), must not be forgotton, nor his re-
mark as to this faulting having taken place previously to the present modification
of the country’s surface. The downthrow is described as at least 40 feet, and
perhaps more. The faults in the Hitchin section have been recognized by Mr.
8. V. Wood, jun., who has drawn them in section No. 6, illustrating his memoir
entitled “Remarks in explanation of the Map of the Upper Tertiaries of the
counties of Norfolk, Suffolk, Essex, Middlesex, Hertford, Cambridge, Hunting-
don, and Bedford, with parts of those of Buckingham and Lincoln, and accom-
panying sections. 1865.”

566 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

pebbles, and ironstone-nodules cemented pretty firmly together, and
passing up into fine yellow sand, laminated and well bedded, and this
again covered by the gravelly loam which lies indifferently upon chalk
or sand. The chalk is fissured, rises in little craggy prominences into
the drift (b), or shows steep short escarpments against which the
chalk-rubble has accumulated. I saw it in this form at Herting-
fordbury a few weeks back.

However, we have only to return to the station, and enter the
bay in the cliff where the lime-kilns are at work, to see the accom-
panying section. South of the gravel-shoot, the chalk descends
rapidly, dipping N. or N.W. to within 10 feet of the road-level, and
is much shattered in the hollow. The fine gravelly sand, underlain
by 2 or 3 feet of conglomerate, follows it; and then, just under
the shoot (which seems put there to protect the section), it is suddenly
faulted to the extent of at least 7 feet, and probably more, showing.
the clean face of a fault which has cut through chalk, chalk- and
flint-pebbles, and gravelly drift, the faces of the faults, three or four
in number, and parallel to each other, being as clearly defined in the
hard drift and conglomerate bed (the pebbles of which are often.
fractured across) as in the chalk itself. The loam and chalk-rubble
mixed descend irregularly into the hollow, and leave generally but
a foot or two of undenuded gravel-drift above the conglomerate.

Section of Chalk, mKe and Upper Gravels at Hitchin Station.

Vy,
WY i
WH I |

Cola a
a. Chalk. b. Drift. e. Pebble-bed. d. Fine gravelly sand.

The section here is so very clear as to admit of no doubt; and I
leave the matter for the consideration of those who are apt to forget
that faults in the drift imply a very recent modification of the surface
by movements similar in kind, if in less degree, to those which produced
our mountain-ranges.

1866. ] WILSON—FCUADOR. 567

5. On some Frint Imptements lately found in the Vatiey of the
Lirttz Ouse River, near Tuerrorp. By J. W. Frower, Esq.,
F.G.S.

(The publication of this paper is unavoidably deferred.) -

[ Abstract. ]

Tue sands and flint-gravel on the right bank of the river Ouse at
Thetford form a terrace 8 to 10 yards above the river, and about
40 yards distant from it. At a spot called Red Hill a large number
of flint implements have lately been obtained from this gravel, at
from 12 to 15 feet below the surface, and within a foot or less of the
chalk on which the gravel rests; and some were found in the same
gravel filling pot-holes in the chalk.

The author pointed out the exact correspondence, as regards geo-
logical position and relations, between the Thetford gravels and the
flint-implement-bearing beds of Amiens, Abbeville, Fisherton, Ick-
lingham, Hoxne, &c. He further noticed the close resemblance
which these implements and some others discovered in England
bear to those of the valley of the Somme; and concluded by ex-
pressing his dissent from Mr. Prestwich’s conclusions, and stating
his own views on their mode of accumulation, remarking that, in
his opinion, these implements were manufactured prior to the sever-
ance of this island from the continent.

6. Grotoeicat Novus of the Pactric Coast of Ecvavor, and on some
Evivences of the Antiquity of Man in that Rueton. By J.S.
Witson, Esq.

(Communicated by Sir R. I. Murchison, Bart., K.C.B., F.R.S., F.G.S.)
[ Abstract. |

Tue western slope of the Cordilleras is occupied with projected
volcanic matter, presenting an irregular aggregation of boulders,
gravel, sand, fine earthy matter, or ashes, and pumice. The boulders
are of various sizes, and consist principally of the more ancient and
the hardest plutonic rocks. Small angular fragments of granite are
occasionally met with many miles from where that rock is found at
the surface, and where there exists no evidence of their having been
transported by water.

In some of the older strata of this volcanic rock, extending along
the coast and some distance inland, occur cavities, that have been
once occupied by the roots of trees, in their original place alongside
prostrate stems, which indicate that there were periods of repose of
the volcanic agencies by which the materials constituting this rock
were distributed. Traces of forest-vegetation in the volcanic mate-
rial were found on the coast and in some of the older beds of that
deposit, commonly below high-water mark, and also at various
points up the river Esmeraldas, and at all altitudes up to the foot

VOL. XXII.—PART I. 2a

068 PROCEEDINGS OF THE GEOLOGICAL SOCEETY. [June 20,

of Pichincha. In this latter locality, and in beds of more recent
date than those which extend to the coast, roots and stems of small
trees, completely carbonized, have been found, some descending to the
depth of 100 feet below the surface. Whilst the trees in this latter
locality, though of more recent production, are converted into perfect
charcoal, those of the older volcanic deposits are not at all carbon-
ized. And, again, the wood of the buried forest at the mouth of the
Esmeraldas, lying only 12 to 15 feet under beds of an estuarine clay,
and much more recent than either of the above, is partially carbon-
ized, and resembles lignite. It is the author’s opinion, in regard to
the charred wood in the vicinity of Pichincha, that, as the ashes
and dust thrown out by that volcano fell in dense showers over
the surrounding country, the heat still retained by this matter car-
bonized the trees which it enveloped and buried.

It is beneath this voleanic deposit, cr in some of its lowest beds,
that the gold-drifts are found, as at Playa de Oro, Cachibi, at Bar-
bacous, New Granada, &c. And it is only when this deposit has
been removed, or where ancient river-courses have been again pene-
trated by waters of more recent times, that gold is found in this part
of Keuador and the adjoining part of New Granada.

The projected volcanic matter is distributed in terraces, the most
recent of which extends along the shores of the Esmeraldas, and is
but slightly above high-water mark. The second rises in some places
10 feet above the former, and is extensive at the lower part of the
Esmeraldas and up the valleys of its lower tributaries. A third,
presenting a distinct margin, rises about 8 feet higher; and above
this rise three other terraces, respectively, in their orders of ascent,
15, 12, and 6 feet. This is the arrangement which (with the ex-
ception of the lowest and therefore the most recent terrace) is clearly
defined in ascending the north side of the river Esmeraldas from oppo-
site the river Viche to the Quebrada of Chancama (see section). At the
former place the terraces recede from the river to an undetermined
distance, but which is evidently extensive, and are said to reach to the
Rio Verde, which receives a portion of the drainage from them: this
seems the more probable, as but an inconsiderable amount of the
water falls into the Esmeraldas. ~The series of terraces is again
met with in the road above the mouth of the river Sadi, their con-
tinuation being partially broken by the projection of a range of hills.
It is observable in this locality that the river has cut its way deep
across the terraces, and in many places completely through the vol-
canic matter, and regained its more ancient bed on the Carboniferous
rocks.

Rocks of Tertiary age are represented in the limestone cliffs,
resting on shale, north of the Rio Verde, and at the side of the river
Esmeraldas, just above the old town of that name, where the lime-
stone is overlain with the volcanic deposits. Again, the Tertiary
limestone was found much further up, where the river passes through
a range of hills in the vicinity of the river Caninde ; here it appears
by the river-side in enormous white angular blocks, which had
evidently fallen from the side of the precipitous hill behind: the

1866. ] | WILSON—ECUADOR. 569

limestone appeared to rest on the volcanic deposits, and it was the
washing away of this latter from underneath that caused the harder
limestone to break off in those enormous blocks. So far as the
author’s observations yet extend, the earlier beds of the volcanic
material are at least contemporaneous with the Tertiary limestone ;
and the accumulation of these volcanic outcastings continued until
long after the close of the Tertiary period, but became gradually more
circumscribed.

Section of Point at Chancama.

oe ee Ouenradaior
Chancama

Sand and gravel.

a. Vegetable mould. é.

6. Clay and sand with pottery. f. Trash-rock.

c. Water-worn gravel and clay with | g. Blue slaty rock with fragments of
pottery. shells.

d. Gravel and clay with pottery.

The second of the terraces described contains, in many places,,
remains of articles of human art (broken pottery, earthen figures,
and fragments of gold ornaments) at various depths below the

“surface, but in all cases below high-tide mark, from which fact it is
apparent that this region, during its occupation by man, stood
higher above the sea than it does now. But the sea gradually en-
croached on the land, till it attained a height of about fifteen feet
above its former level. That the duration of time occupied by this
advance and retreat of the sea must have been very great is apparent
when we consider that the stratified earth of the plain is simply
the sediment brought down by the rivers and deposited beneath the
margins of the sea, in some places to the depth of ten feet above the
surface on which the ancient cities stood. Again the land sank and
deposited those low flats and islands found at different places along
the sea-margins. The land is again gradually sinking.

The pottery-stratum is traceable along a line of 80 miles of coast,
and, by partial observations, is determined to occur under corre-
sponding conditions for a distance of 200 miles more.

_ The discovery of pottery in a formation considered by the author

immensely older than. the clay-beds of the coast, in the uppermost,

excepting one, of the terraces described, was made at Chancama,
292

570 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

situated 24 miles from the coast, 180 feet above the sea, and 50 feet
above the Esmeraldas river. The section (see fig.) exhibits undis-
turbed sea-distributed gravel and sands, 6 feet 6 inches in thickness,
the lower part of which contains fragments of pottery.

7. On the Retations of the Tertiary Formations of the West INDIEs.
By R. J. Lecumere Guppy, Esq., F.G.S. With a Note on a New
Species of Ranina, by Henry Woopwarp, Esq., F.G.S.; and on
the OnprrorpEes and Nummvu.in#, by Prof. T. Rupert Jonus, F.G.S.

(Abridged.)
[Puate XXVI.]
ConrENTS.
I. The Paleontology of the Cari- 5. The age of the Caribean
bean Area. Miocene.
1. Introduction. 6. Other Tertiary Formations
2. Eocene Formations. in the West Indies.
3. Lower Miocene Formations. II. Descriptions of the species.
a. Trinidad. c. Antigua. III. The relations of the Caribean
6. Anguilla. Miocene Fauna.
4. Upper Miocene Formations. IV. Table showing the Affinities of
a. SanDomingo. ce. Trinidad. some of the Fossils of the Ca-
6. Jamaica. d, Cumana. ribean Miocene.

I. THe PALZontTOLOGY OF THE CARIBEAN AREA.

§ 1. Iyrropvcrion.

Ir may be that some apology is needed for again bringing before the
Geological Society the subject of West-Indian Geology. I should
not, indeed, have ventured to do so, but for the circumstance that the
‘considerations involved do not alone concern the geology of the West
Indies, but have an important bearing on several questions connected
with the distribution of organic beigs in Europe and Asia, and on
the correlation of deposits in those countries. These questions have
much interest for geologists; and I believe that the facts and argu-
ments presented in this communication are such that my labour in
bringing them together will not be lost, even if the hypothetical
views I have built upon them should prove to be untenable. More-
over the present communication forms a necessary sequel to those I
have already had the honour of laying before the Society.

My object now is to present some general remarks on the results
obtained by recent investigations into the geology and paleontology
of the West-Indian islands. But before going into these, it may be
as well that I should review our knowledge of the deposits, begin-
ning with the oldest Tertiary formations.

§ 2. Hocrnr Formattons.

The existence of Eocene strata in Jamaica has been demonstrated
by Mr. Barrett* and by Dr. Duncan and Mr. Wally. Determinable -

* Quart Journ. Geol. Soc. vol. xvi. p. 324. + Lbid. vol. xxi. p. 1.

1866. | _ GUPPY—WEST-INDIAN TERTIARIES. 571

fossils are rare; but three species of corals have been enumerated by
Dr. Duncan, none of which are new.

No strata of ascertained Eocene date have been shown to exist
elsewhere in the Caribean area; but it is probable that some of the
deposits attributed to the Miocene period in Trinidad pass down into
it, as will be mentioned in the next section.

§ 3. Lowrr Mioczye Formations.

Ishall use the terms Lower and Upper Miocene, upon this as upon
former occasions, not as implying equivalency to the Upper and
Lower Miocene of Europe, but merely as marking what seems to
me, at present, the relative age of the formations under consideration.

a. Trinidad.—In this island there is a very extensive develop-
ment of Tertiary formations; and it is exceedingly difficult to refer
all the beds to their proper places in the series, owing to the want of
sections showing their relative position. The Geological Survey of
the West Indies divided them into five groups*. Of these, the strata
exposed at San Fernando, which were probably included in the
‘¢ Naparina Marls,”’ and those classified as the ‘‘ Tamana Series,” seem
to me to be the oldest. The beds at San Fernando consist of gypseous
marls, with shales and irregular limestones, all inclined at a very
high angle. In the annexed section (fig. 1) I have endeavoured to
give an idea of the stratigraphy of the beds, which is very obscure,
owing to the face of the cliff being in great part hidden by slips
from the top.

Fig. 1.—Section at San Fernando (2 mile).

Paradise Gate. Paradise.

AA \\

456789 10

.
'
|

1. Brown clays and marls, sometimes indurated.

2, 3. Gypseous marls, with indurated layers and beds strongly impregnated
with asphalt. Concretions containing fossils converted into selenite.

4. Indurated asphaltic marl.

5. Irregular dark-blue limestone, containing numerous fossils generally con-
verted into calespar, or replaced by semiliquid asphait (Ranina and fish-
teeth).

a. marls, more or less indurated, with occasional fossils ( Orbitozdes, &c.).

Sandstone ( Turritella, Cardium, Nummulina).

Dark indurated marls and shales containing much asphalt.

Orbitoides-bed. Black asphaltic bed consisting chiefly of the shells of Orbitotdes
and Nummulina,

10. Asphaltic and gypseous clays, shales, and marls ( Zerebratula, Hchinolampas,
Trochus, Cardita, Orbitoides, &c., chiefly found in indurated gypseous
layers or nodular concretions).

11. Indurated marls containing much asphalt. Fossils very rare.

12, 14, 16. Blue clays, unfossiliferous.

13, 15, 17. Gypseous marls. Fossils rare and usually imperfect.

sO DAIS

* Report on the Geology of Trinidad, p. 35.

572 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

_ Fig. 2 isa diagram to show the general relations of the above and
other deposits in Trinidad alluded to in this paper.

Fig. 2.— Diagram Section to show the general Relations of the
Formations in Tromdad.

.E. River Mount 8.W.
Northern Ranges. Caroni. Tamana.
t

. “Caribean Group.” 5. “ Caroni Series.” Ugued Nooo
. Neocomian. 6. “Moruga Series.” f ~ PPe® “10cene.
. San Fernando Beds. | Lower Mio- 7. “ Detrital Series.”

He OS be

. “Tamana Series.” cene.

The following is a list of the fossils which have been determined
from the San Fernando beds :—

Natica phasianelloides, D’ Ord. Kchinolampas ovum-serpentis, Guppy.
Terebratula Trinitatensis, Guppy. Spirorbis clymenioides, spec. nov.
—— cameoides, Guppy. Ranina porifera, H. Woodw.,spec. nov.
—— lecta, Guppy. Orbitoides Mantelli, Morton.
Gryphea athyroides, spec. nov. Cisseis asterisca, spec. nov.

Besides these fossils there occur species of Pinna, Arca, Trochus,
Cardita, Lucina, Nummulina, Heterostegina, &c.* Only one of the
Mollusca has been identified with a Miocene species, none with
recent species; and the general affinities of the fossils appear to be
Nummulitic. Ihave for the present retained these beds in the Mio-
cene, because they had been so classified by the Geological Survey.
Mr. Woodward has been kind enough to determine for me the
Ranina, and his note describing the species is appended. It will be
seen that the evidence furnished by the Crustacean is in favour of
the view I have taken of the age of the San Fernando beds.

The beds exposed at Manzanilla Point, on the east coast of Trini-
dad, consist of a succession of sands, caleareous sandstones, and dark
shales. Their stratigraphical relations to the San Fernando beds
cannot be ascertained, as they are deposited on the opposite side of
the ridge of Neocomian strata. The diagram (fig. 2), in which they
are included in the Tamana series, shows their general position; and
I have added a section (fig. 3) to make their stratigraphy more clear.
' The beds which are seen on the coast at Manzanilla seem to pass on
the north under strata assigned by the Geological Survey to the Caroni
(Upper Miocene) series; but it is not quite clear whether the pas- -
sage is conformable or not, owing to the swamps which occur near
the junction in the coast section. To the south the extension of the
series is hidden by the detrital (post-tertiary) deposits and by the
Nariva swamp. The beds may be traced inland for a distance of
four miles, when they end abruptly and unconformably on the Neo-
comian rocks. As the organic remains collected by the Survey have
not been described, I cannot affirm that the deposits classified by

* Geologist, vol. vii. (1864) p. 160; and Quart. Journ. Geol. Soc. vol. xxii. p. 295.

1866.] - GUPPY—WEST-INDIAN TERTIARIES. 573

them in the Tamana series all belong to the same horizon as the
Manzanilla beds. There does not, however, appear to be any reason
on stratigraphical grounds why these latter, with the San Fernando
‘beds, should not be older than the other Tertiaries of Trinidad.

Fig. 3.—Section from Nariva Swamp to Mount Calabash,
32 miles from the coast (6 miles). ©

» §.8.W. Mount River Mount N.N.E.
Nariva Swamp. Lebranche. Lebranche. River. Calabash.
; } P

a, Clays and shales (Caroni series).
6. Clays, calcareous sandstones, &c. (Manzanilla beds).
e. Sandstone and indurated clays (Neocomian).

Their organic contents seem to consist of a different assemblage of
species to that found in the other Miocene deposits, containing at
the most, out of more than thirty species of Mollusca collected by
me, but four found elsewhere. Consequently I place these forma-
tions, provisionally only, in the Lower Miocene until further evi-
dence may be forthcoming as to their true age.

The fossils from the Manzanilla beds which are now described,
consist of the following species :—

Ancillaria lamellata, spec. nov. Cercomya ledzeformis, spec. nov.
Venus Walli, spec. nov. Erycina tensa, spec. nov.
Dosinia cyclica, spec. nov. Arca Trinitaria, spec. nov.
Mactrinula macescens, spec. nov. filicata, spec. nov. ~

Corbula vieta, spec. nov. Cardium castum, spec. nov.

Of the above, the Ancillaria somewhat resembles A. glandina of
the Paris and London basins. Dosinia cyclica is a remarkable form,
connecting the genera Dosimea and Cyclina. Mactrinula macescens is
distantly related to M. pretenuis (Conrad) of the American Eocene,
and more closely to M. plicataria, a living species of the Indian seas.
Corbula vieta occurs in the Miocene of Jamaica and the Pliocene of
Trinidad. It is allied to C. gibba and C. pisum of the Hampshire,
Isle of Wight, and Belgian Tertiaries. Hrycina tensa strongly re-
sembles a Paris-basin species. With regard to Cercomya ledeformis,
if I have rightly determined the generic relations of that shell, it
will be the first recorded appearance of the genus in beds of so late a
date. Among the undetermined shells are a Strombus and a Pleuro-
toma, which are possibly identical with species from San Domingo
and Jamaica; but as the specimens are imperfect I do not venture
to name them.

b. Anguilla.—The Miocene strata in this island consist of a white
marly limestone containing a large number of Mollusca and Echino-
dermata, the former mostly in the state of casts and specifically in-
determinable. The Echinodermata are better-preserved. Ihave no
data as to the position of the beds; but it is worthy of remark, in
respect to the influence of the conditions of mineralization upon the
remains preserved in the rocks, that in Anguilla, where the deposits

574 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

seem to resemble in composition those of Malta, we have an analo-
gous fauna in a very similar state of preservation. In both cases
the Echinoderms are numerous, large, and well-preserved, and
they are accompanied by the teeth of Pycnodont fishes. The
Mollusca, on the other hand, occur chiefly as casts. Could we
find well-preserved examples of the shells occurring at Malta and
Anguilla, they might present us with a closer resemblance between
the faunas of these localities than has as yet been established for
any of the groups of Mollusca found fossil in the West Indies and
in Europe.

The remains determined from the Anguilla beds belong to the fol-
lowing species * :—

Natica phasianelloides, d@’ Ord. Clypeaster ellipticus, Mich.
Solarium quadriseriatum, Sow. Echinolampas semiorbis, Guppy.
Ficula carbasea, spec. nov. —— lycopersicus, Guppy.
Pecten Mortoni, Ravenel. Echinoneus cyclostomus, Leske.
Orbitolites complanatus, Lam. Schizaster Scillz, Desmoulins.
Cidaris Melitensis, Wright. Brissus dimidiatus, Agass.

Kchinometra acufera, Blainv.

c. Antigua.—Details of the strata in Antigua have been furnished
by Nugent? and Dr..Duncant. The latter has described several
corals, besides giving a summary of the geological features of the
Miocene formation in the island.

§ 4. Upper Miocene Formations.

a. San Domingo.—In the northern part of San Domingo there is
an extensive development of Miocene formations, consisting chiefly
of greenish or bluish sandy shales overlain by beds of shingle and
limestone. None of these beds seem to have suffered the great dis-
turbances which have affected the formations in Jamaica and Trinidad,
and the usual dip is only 6° or 7°§. <A large number of Mollusca
and Zoophytes have been obtained from the blue shales, most of
which have been described, the Mollusca by Messrs. Carrick Moore
and Sowerby ||, and the Corals by Dr. Duncan§]. The entire thick-
ness of the series as given by Colonel Heneken does not seem to
exceed 600 or 700 feet. The following are the Mollusca :—

Cassidaria levigata, Sow. Conus symmetricus, Sow.
Cassis sulcifera, Sow. —— stenostoma, Sow.
Oniscia Domingensis, Sow. —-— planiliratus, Sow.
Strombus pugilis, Linn. —— marginatus, Sow.
ambiguus, Sow. —— Domingensis, Sow.

—— Haitensis, Sow. solidus, Sow.

—— proximus, Sow. catenatus, Sow.

—— bifrons, Sow. —— interstinctus, Guppy.
Conus Haitensis, Sow. consobrinus, Sow.

* Quart. Journ. Geol. Soc. vol. xxi. p. 298.

+ Geol. Trans. Ist ser. vol. v. p. 459.

+ Quart. Journ. Geol. Soc. vol. xix. p. 408, and vol. xx. p. 20.
§ Heneken, Quart. Journ. Geol. Soc, vol. ix. p. 115.

|| Quart. Journ. Geol. Soc. vol. vi. p. 39, and vol. ix. p. 129.
q Jbid. vol. xix. p. 406, and vol. xx. p. 20.

1866. | GUPPY—WEST-INDIAN TERTIARIES. 579

Conus gracilissimus, Guppy.
Murex Domingensis, Sow.
Typhis alatus, Sow.
Persona similima, Sow.
Triton variegatus, Lam.
—— femoralis, Linn.
gemmatus, [eeve.
Oliva cylindrica, Sow.

—— hispidula, Lam.

Mitra Henekeni, Sow.
varicosa, Sow.
Fasciolaria semistriata, Sow.
intermedia, Sow. —
Turbinellus ovoideus, Kzen.
validus, Sow.
Haitensis, Sow.
Latirus infundibulum, Ged.
Fusus Henekeni, Sow.
Haitensis, Sow.
Pyrula melongena, Linn.
Marginella coniformis, Sow.
Cyprxa Henekeni, Sow.
—— pustulata, Lam.
Voluta pulchella, Sow.
—— soror, Sow.
Columbella Haitensis, Sow.
—— venusta, Sow.

Cancellaria leevescens, Guppy.

Barretti, Guppy.
—— Moorei, Guppy.
Pleurotoma Henekeni, Sow.
venustum, Sow.
consors, Sow.

—— Haitense, Sow.
Jaquense, Sow.
Terebra flammea, Lam.
sulcifera, Sow.

Terebra ineequalis, Sow.

——- bipartita, Sow.

Phos Moorei, Guppy.

—— elegans, Guppy.

Nassa incrassata, Mil.
Cerithium plebeium, Sow.
—— uniseriale, Sow.

Natica subclausa, Sow.

sulcata, Born.
phasianelloides, D’ Ord.
Solarium quadriseriatum, Sow.
Dentalium Mississipense, Conr.
Petaloconchus scul pturatus, Lea
Vermetus papulosus, Guppy.
Bulla striata, Brug.
paupercula, Sow.
granosa, Sow.

Corbula viminea, Guppy.
Venus Paphia, Linn.

—— puerpera, Linn.

Lucina Pennsylvanica, Linn.
tigrina, Zinn.

Tellina biplicata, Conr.
Cardita scabricostata, Guppy.
Cardium Haitense, Sow.
Pectunculus acuticostatus, Sow
Arca patricia, Sow.

—— Nox, Linn.

consobrina, Sow.

—— pexata, Say.

Pecten Thetidis, Sow.
inzequalis, Sow.
oxygonus, Sow.
Spondylus bifrons, Sow,
Chama arcinella, Lam.

Ostrea virginica, Gmel.

Teredo fistula, Zea.

There are several undescribed species in the Geological Society’s
collection.

b. Jamaica.—As I have so recently given an account of the Mio-
cene Mollusca of Jamaica*, I need do no more than give the names
of some additional species. These are :—

- Turritella tornata, spec. nov. Nezra costellata, Desh.t
Corbula vieta, spec. nov. |

The Corals of the Miocene deposits of Jamaica have been described
by Dr. Duncant. Three species of Echinoderms are known from the
-Tertiaries of Jamaica: they have been named by Michelin; but one
only (Clypeaster ellipticus) has been described or figured.

e. Trindad.—I have alluded to the Caroni series in my paper on
the Jamaican fossils. Its relation to the other Tertiaries is shown
by the diagram (fig. 2). Further particulars will be found in the
‘Geological Report on Trinidad’§; and it is only necessary now to

* Quart. Journ. Geol. Soc. vol. xxii. p. 281.

+ I learnt the occurrence of this shell in Jamaica from Mr. J. Gwyn Jeffreys.
~ Quart. Journ. Geol. Soc. vol. xxi. p. 1.

§ Wall and Sawkins, Geological Report on Trinidad, p. 41.

576 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

give a list of the fossils determined by me. The Moruga series is
classified with the Caroni series by the Geological Survey of the West
Indies; but I have no information as to its fossil contents, beyond the
list of genera given in the Report. The following species are from
the Caroni series at Savanetta on the Parian side of the island :—

Turbinellus ovoideus, Kien. Pecten oxygonus, Sow.

Solarium quadriseriatum, Sow. comparilis, Tuomey § Holmes.
Petaloconchus sculpturatus, Lea. Ostrea virginica, Gmel.

Dosinia acetabulum, Conrad. Ficula carbasea, spec. nov.

Tellina biplicata, Conrad. Teredo fistula, Lea.

The Mollusca occur generally of large size. Several of the unde-
termined species resemble shells from San Domingo; but their con-
dition is such as to render it unsafe to give the names.

Numerous seams of coal occur in the series, some of which, being
of workable thickness (3 to 4 feet), may eventually prove of use.
There are at present no facilities for getting at the coal, owing to the
want of roads and paucity of inhabitants in that part of the country
where the beds are exposed.

d. Cumana.—I have already alluded to the nature of the beds
containing Miocene fossils at Cumana on the north coast of Vene-
zuela*. Further particulars will be found in Mr. Wall’s communi-
cation “ On Venezuela and Trinidad.” t The fossils have not hitherto
been determined ; but a list of the genera will be found in the Ap-
pendix to the Geological Report on Trinidadt. The following is a
list of the species which I have been able to determine :—

Pyrula melongena, Linn. Melanopsis cepula, spec. nov.
Murex Domingensis, Sow. Turritella torn&ta, spec. nov.
Persona simillima, Sow. Turbo castaneus, Gmel.
Fasciolaria Tarbelliana, Graz. Natica suicata, Born.
Columbella venusta, Sow. Bulla striata, Brug.

Conus gracilissimus, Guppy. Venus Paphia, Linn.

Woodwardi, Guppy.

symmetricus, Sow.
cancellata, Linn.

Oliva hispidula, Lam.

cylindrica, Sow. Cytherea juncea, spec. nov.
Marginella coniformis, Sow. —— convexa, Say.
—— interrupta, Lam. Lucina Pennsylvanica, Linn.
. Cancellaria Moorei, Guppy. —— tigrina, Linn.
Terebra inzequalis, Sow. Cardium Haitense, Sow.
Pleurotoma Haitense, Sow. _ Pectunculus pennaceus, Lam.

—— Barretti, Guppy. — acuticostatus, Sow.
Phos elegans, Guppy. Arca consobrina, Sow.
Nassa solidula, spec. nov. pexata, Say.
Cerithium plebeium, Sow. incongrua, Say.
—— uniseriale, Sow.

From this list, which must be regarded as a provisional one, it
will be seen that the proportion of recent species (39 per cent.) is
greater than has been determined for any of the other Caribean Mio-
cene deposits. This may be partly due here, as elsewhere, to the
facility with which I have been able to identify recent species. Of
the fourteen recent species, only three have not been recorded from
other West-Indian Miocene beds. Of the total of thirty-seven spe-

* Quart Journ, Geol. Soe. vol. xxi. p. 282.
t Jbid. vol. xvi. p. 460. t Report, &c. p. 163.

—

1866. ] GUPPY—WEST-INDIAN TERTIARIES. 577

cies, nineteen have been found in Jamaica, and twenty-five in San
Domingo, leaving but seven now enumerated for the first time from
the Caribean Miocene. From this analysis it will be seen that it
would be difficult to separate the Cumana beds from the Caribean
Miocene, and at the same time that it is probable they represent
one of the highest stages of that formation.

§ 5. Tue Acs or THE CarIBEAN MIocENE.

The affinities of the organic remains of the Caribean Miocene are
stronger with foreign species, both Midtertiary and Recent, than
with the existing fauna of the West Indies, indicating an antiquity
somewhat greater than would be adduced for them from the propor-
tion of extinct species, which I cannot consider greater for those
deposits I have classed as Upper Miocene than 80 per cent. In my
paper on the Jamaican fossils [ showed that the proportion of recent
species was 20 per cent. ; and by comparing the list I have given of
the San Domingan Mollusca, it will be seen that a similar proportion
obtains for them. In explanation of the discrepancies between my
list and previous estimates, I may remark that I cannot consider the
Pyrula consors of Sowerby to be distinct from the P. melongena of
Linné, nor the Ostrea Haitensis of Sowerby to be specifically distin-
guishable from the O. virginica of Gmelin. Mr. Carrick Moore, in
the latter of his papers on the San Domingan fossils, reduced the pro-
portion of living species to 8 or 9 per cent.; but this was done by
assigning certain of them to deposits of a later period. However, as
those species haye been found in Jamaica and elsewhere associated
with the characteristic fossils of the Caribean Miocene, I have not
felt myself justified in excluding them from the Haitian list.

§ 6. Orger Tertiary Formations In THE West InpDIEs.

There exists in several of the West-Indian islands undoubted later
Tertiaries containing a very large proportion of recent species. This
seems to have been partly the cause of the confusion as to the age
of some of the fossils. Our knowledge of the geology of these islands
being so limited, some authors have inferred that all the fossils were
derived from the same formation. It is often difficult to distinguish
between the rocks composing the newer and older formations, both
being sometimes white calcareous deposits, and the newer frequently
being the hardest.

The Tertiary formations of Guadeloupe have been studied by
Duchassaing, who divides them into Newer and Older Pliocene and
Miocene*. To the first of these are assigned, amongst other depo-
sits, those containing human remains. From the Older Pliocene
Duchassaing obtained twenty-six species of Mollusca, many of which
he identified with recent speciesf. He records from the same beds
thirteen Echinoderms, of which seven are extinct. It would seem
that these results are somewhat discordant; and when we consider

* Bull. Soc. Géol. de France, sér. 2. vol. iv. (1847) p. 1093.
t Ibid. sér. 2. vol. xii. p. 753.

578 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

that some of the Mollusca are identified with European Hocene spe-
cies, it is obvious that we cannot consider our knowledge of the
Tertiaries of Guadeloupe at all exact. In Duchassaing’s list eight
corals are mentioned. Dr. Duncan has also treated of the fossil
corals of Guadeloupe*.

Duchassaing refers centain deposits to the Miocene. From the
lower volcanic sands, which he includes in this formation, he only
gives us the names of two Mollusca, one of which he considers to be
identical with a Paris-basin species, and the other occurs in his
Older Phocene. According to Moreau de Jonnést, the Miocene
formation includes Terebratule like those of more ancient strata. If
this is the case, it may be the equivalent of the San Fernando beds
in Trinidad.

M. Payen found fossils in Guadeloupe referable to Cyprea, Tere-
bratula, Spatangus, and Hchmus. Deshayes considered these to be
Quaternary, and the Z’erebratula to belong to a new speciest.

In Trinidad, beneath a large unfossiliferous detrital series, there
exists a Pliocene formation, exposed at Matura on the east coast,
from which I have already published a list of species§. Many of
my determinations were doubtless erroneous; but to provide for
mistakes of this kind I affixed marks to such of the species as I had
compared and found identical with recent forms. I see no ground
for changing my opinion as to the relative age of these beds, although
it is probable that the percentage of extinct species is somewhat
greater than stated.

The greater part of the island of Barbados appears to consist of
Tertiary rocks which have been divided into two main divisions.
The newest of these, the coral-limestone, contains a large number of
recent species. No extinct species of Mollusca are recorded from it.
The Scotland formation is considered to be older, and the following
shells have been described from it]|| :-—

Scalaria Ehrenbergi, Forbes. | Nucula Schomburgki, Forbes.
Nucula Packeri, Forbes.

This formation was considered to be Miocene by Professor Forbes ;
and it seems to include the deposits containing siliceous organisms J.
Dr. Duncan has described, in his paper before cited, three species of
corals from Barbados.

Barbuda contains a formation resembling the coral-limestone of
Barbados. It consists of a white calcareous deposit full of shells, all
of which are, as far as I have examined, of existing species. The
existence of a Miocene formation in that island seems, nevertheless,
to be indicated by the corals described by Dr. Duncan. That palee-
ontologist has also described corals from Montserrat Ge.

* Quart. Journ. Geol. Soc. vol. xix. pp. 412, 452.

+ Cited by Duchassaing, Bull. Soc. Géol. France, sér. 2, vol. iv. p. 1093.

* Bull. Soc. Géol. de France, sér. 2. vol. xx. (1863) p. 475.

§ Geological Magazine, vol. ii. (1865) p. 256.

|| Schomburgk, History of Barbados, p. 565.

q Ebrenberg’s account of these fossils was partly translated in Ann. Nat. Hist.
vol. xx. p. 115.

1866. | _ GUPPY—WEST-INDIAN TERTIARIES. ~ 579

D’Orbigny has published figures of a number of fossils from Cuba,
which he identifies, for the most part, with recent species* ; but as
they are all casts, it is difficult to place reliance on the determina-
tions. Two of his species I have recognized in the Miocene beds of
Jamaica, San Domingo, and Trinidad. One of these is the Natica
phasianelloides, and the other is Tellina Sagre, which seems to me
identical with 7’. beplicata of Conrad.

Beyond some general notices scattered through various works, I
believe but little more is known of the geology and paleontology of
the West Indies than I have indicated. The present summary,
though not, perhaps, of much interest as far as it relates to the
later Tertiaries, will be of service to future investigators of West-
Indian geology tr.

II. Descriptions oF THE New Specizs.
1. Nassa SOLIDULA, spec. nov.

Shell turreted, thick, costated by stout distant rounded ribs, which
are almost developed into tubercles on the angle of the whorls, and
are cancellated by numerous fine and close spiral costelle, of which
there are usually two finer in the interval between two larger ones;
spire conical, sharp; whorls 8, somewhat angulate above, the last
much larger, forming two-thirds of the length of the shell; outer
lip dentate, thickened externally, forming a varix ; columellar margin
with a narrow callus; columella strongly twisted; canal short,
abruptly reflected.

This form is related to V. prismatica, Brocchi; but there are con-
siderable differences, among which are the relative narrowness of
the present shell and its sharper spire.

Locality.—Cumana, Upper Miocene.

2. ANCILLARIA LAMELLATA, spec. NOY.

Shell ovate-conic ; spire elevated, acuminate, spirally striated ; last
whorl rather ventricose, spirally striate above ; aperture suboval,
elongate ; columellar margin rather strongly folded and bearing a
lamellar parietal tooth or pled, which extends into the interior, ob-
structing the posterior part of the aperture.

* Paléontologie de Cuba.

+ Besides the various memoirs already cited, the A llovins will be found in
the publications of the Geological Society :—

Bahamas.—Nelson, Quart. “Journ. vol. ix. p: 200.
‘Barbados.—Skey, Geol. Trans. Ist ser. vol. iii. p- 238 ; Ehrenberg, Quart.
Journ. vol. iv. pt. 2. p. 19. :
Bermuda.—Vetch, Geol. Trans. 2nd ser. vol. i. p. 172; Nelson, Geol. Trans.
2nd ser. vol. v. p. 103.

Jamaica.—De la Beche, Geol. Trans. 2nd ser. vol. ii. p. 143; Owen (On a
Fossil Mammal), Quart. Journ. vol. ii. p. 541.

Montserrat.—Nugent, Geol. Trans. Ist ser. vol. i. p. 185.

Trinidad.—Nugent, Geol. Trans. Ist ser. vol. i. p. "63,

Jamaica.—Sawkins, Quart. Journ. vol. xix. p. 35.

With the exception of those by Owen and Ehrenberg, the above papers relate
chiefly to the physical and mineralogical structure of the islands.

580 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

This shell, near in general shape to A. glandina, is distinguished
by the enamel which is spread over the spire being regularly and
distinctly spirally striated or grooved, and by the strong parietal plait.
In some examples the spiral grooving covers the whole of the whorls ;
but in others the greater part of the last whorl is smooth. The
columella is grooved in a similar manner.

Lower Miocene, Manzanilla, Trinidad.

3. FICULA CARBASEA, Spec. Nov.

Shell pyriform, somewhat ventricose ; spire short, scarcely elevated;
whorls 5, ornamented with equidistant raised spiral lines, of which
there are three finer between every two of the larger lines, their
interstices being cancellated by numerous fine subequal raised lines,
which scarcely rise upon the spiral ones; suture sunk; aperture
ovate, wide, nearly as long as the shell. |

This species closely resembles F. clathrata, Lam., from which it is
distinguishable by the ornamentation.

Trinidad (Caroni Series); Anguilla.

4, MELANOPSIS CAPULA, Spec. nov.

Shell ovate-turreted ; spire conical, sharp; whorls about 7, regu-
larly increasing, ornamented superiorly with fine coste, becoming
obsolete on the last whorl, which forms more than half the length of
the shell; suture linear, impressed; aperture ovate; outer lip sim-
ple, prominent; collumella twisted; canal short and broad.

I do not know of any form resembling this species, which was
probably not a freshwater shell. It may possibly have been an
estuarine form. It reminds one of a shortened and widened Hulima,
or even a Stylifer.

Upper Miocene, Cumana.

5, TURRITELLA TORNATA, Spec. Nov.

Shell turreted, elongate; whorls numerous, increasing very gra-
dually, ornamented with two spiral keels, each bearing a monili-
form row of granules; the upper keel accompanied by a granular
line halfway between it and the linear suture; the rounded conca-
vity between the keels having also two fine linear aa rows of
moniliform granules ; aperture subquadrate.

Upper Miocene, Cumana; Jamaica; San Domingo.

6. CoRBULA VIETA, spec. nov.

Shell subtrigonal, nearly equilateral, rounded at both extremities,
scarcely truncate posteriorly ; right valve turgid, ornamented with
numerous stout, rounded, concentric cost ; umbones prominent.

This shell is variable as to height, small examples approaching in
form to C. elevata, Conr. It appears to be most closely allied to
CO. gibba and C. pisum, from which it is distinguished by its greater
size and stouter concentric ribs, of which there are between thirty
and forty on the large valve of well-grown examples of C. vieta. It
is also less truncate posteriorly than the species mentioned.

1866. | GUPPY—WEST-INDIAN TERTIARIES, 581

Lower Miocene, Manzanilla, Trinidad; Upper Miocene, Jamaica.
It also occurs in the Pliocene of Trinidad.

7. CERCOMYA LEDAFORMIS, spec. nov.

Shell transverse, elongate, inequilateral, thin, closely covered with
numerous fine and regular longitudinal or concentric ridges; ante-
riorly rounded; posteriorly produced into a pointed rostrum, of
which the upper margin is concave; posterior cardinal area strongly
impressed.

In addition to the strong ridge defining the cardinal area a second
ridge runs from the umbo to the end of the rostrum, upon which, in
some examples, the concentric ridges rise into small points.

I have not been able to observe the details of the hinge of this
shell. The right valve alone has occurred to me in a moderately
perfect state; but fortunately I have discovered some shattered left
valves, which prove that this shell is not a Pandora with a flat left
valve, which I at first imagined it might be. I have therefore con-
sidered it to belong to the genus Cercomya, which has not hitherto
been recorded from Tertiary rocks.

Lower Miocene, Manzanilla, Trinidad.

8. MacrRINULA MACESCENS, spec. nov.

Shell oblong-subtrigonal, thin, compressed, nearly equilateral, with
broad transverse sulcations, which begin at the keel-like ridge on
the posterior margin, and are continued to the rounded and somewhat
produced anterior margin; umbones small, depressed; posterior
marginal area separated by an acute keel, extending from the umbo
to the angle of the inferior margin; hinge with a double cartilage-
pit and a A-shaped cardinal tooth in the left valve; laterals in the
same valve lamellar, forming a deep groove for the ligament ; laterals
in the right valve lamellar, doubled; cardinal tooth obsolete.

_ The nearest recent ally of this shell is WM. plicataria, Linn., which
is an inhabitant of the Indian Ocean. It is more distantly related
to M. pretenwis, Conrad, of the Eocene deposits of North America.

Lower Miocene, Manzanilla, Trinidad.

9. Venus WALLI, spec. nov.

Shell subtrigonal, somewhat inequilateral, anteriorly rounded,
posteriorly somewhat angular, ornamented with numerous small and
fine close radiating costelle, interrupted by high concentric crenu-
late ridges, which are higher and closer towards the ventral margin;
umbones small, prominent; lunule impressed, sinuately striated,
circumscribed by a sharp groove; posterior cardinal area distinct,
striate.

On the disk the costelle are distinctly paired, with a smaller
intermediate costella between each pair; but near the keel which
runs from the umbo to the posterior angle, separating the striate
posterior margin, the costelle are larger and single, and the concen-
tric ridges die away into the striations.

This species is related to the recent V. cancellata.

Lower Miocene, Manzanilla, Trinidad.

582 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

10. CyTHEREA JUNCEA, spec. nov.

Shell subtrigonal, rounded anteriorly, and somewhat angular and
truncate behind, ornamented with numerous thin concentric lamelle,
alternately rather higher; posterior cardinal area slightly folded,
rather indistinct ; lunule impressed, striated ; umbo small, incurved ;
hinge-teeth strong, the hinder (of the right valve) bifid, the two
anterior ones compressed, close together, and having before them a
deep oblong pit for the reception of the tooth of the opposite valve.
Hinge-area with a long groove extending from the termination of
the ligament nearly to the posterior angle.

Upper Miocene, Cumana.

11. Dosrtnta cycrica, spec. nov.

Shell nearly orbicular, thick, subinequilateral, scarcely swollen,
finely and regularly concentrically striated, with occasional deeper
subrugose lines of growth towards the ventral margin; umbones
small, compressed, and closely approximate; lunule entirely wanting ;
margins plain. Hinge consisting of a broad flat plate circumscribed
by the raised dorsal margin; teeth three, large; the central and
largest one placed immediately under the umbo; the other two
lamellar and divergent, the posterior one largest. :

- This shell has the general shape of Dosinia discus. It is also
allied to D. orbicularis of the Bordeaux deposits. It wants the
lunule and the small anterior tooth ascribed to the genus Dosinia,
and I thought at first of referring it to Cyclina. The general
character of the hinge, as well as of the exterior, however, resembles
that of D. orbicularis so closely that I have decided to place it under
the same generic name as that species. It is evidently intermediate
in some respects to the two genera mentioned. It is readily distin-
guished from D. acetabulum, another species to which it bears some
resemblance, by the very different arrangement of the hinge-teeth,
by the total absence of a lunule, and by the umbo being less in-
curved.

Lower Miocene, Manzanilla, Trinidad.

12. CarDIUM CASTUM, spec. nov.

Shell subovate, somewhat oblique, ventricose, ornamented with
about twenty-two stout, rounded, radiating ribs, imbricated by
numerous transverse striz, which are continuous across the inter-
stices ; umbones small, prominent; posterior margin divided from the
disk by a rounded carination ; margins pectinate.

Allied to the recent C. obovale, Sow. In young examples the
difference in size of the ribs on the disk and those on the posterior
margin is more marked, and gives a strongly carinate appearance to
the shell, which is scarcely so conspicuous in larger specimens.

Lower Miocene, Manzanilla, Trinidad.

13. Erycrna TENSA, Spec. nov.
Shell ovate, subequilateral, minutely striated concentrically with

about fourteen low and somewhat distant radiating ribs; anteriorly
rounded, posteriorly truncate ; umbones not prominent.

1866. | GUPPY—WEST-INDIAN TERTIARIES. 583

I do not know of any recent or fossil West-Indian species at all
resembling this shell, which seems to be related to H. obliqua,
Caillat (Z£. nitidula, Desh.), of the Paris basin.

Lower Miocene, Manzanilla, Trinidad.

14. Arca TRINITARIA, spec. nov.

Shell solid, subtriangular, oblique, rather inequilateral, with about .
forty unarmed ribs, which occasionally become imbricated towards
the ventral margin; umbones prominent, curved, separated by a
ligamental area with grooves corresponding to the anterior hinge-
teeth ; posterior margin nearly flat, cordate, divided from the disk
by an abrupt angular carination; anterior edge short, rounded ;
ventral edge nearly straight; inner margin strongly dentate.
Hinge- teeth numerous, lamellar, the lateral ones bent into an angle.

Allied to A. ponderosa, Say. It may easily be distinguished by
the number of ribs and by other characters. It may possibly have
been confounded with A. incongrua by the Geological Survey ; but it
is very distinct from that species. A. Triitaria may be distinguished
from all other Arks with which I am acquainted by the strong angu-
lar posterior ridge and flat posterior margin, which give so peculiar
an appearance to the shell. The lateral hinge-teeth, which are bent
into the form of an L, also afford a good character for the distinction
of this species.

Lower Miocene, Manzanilla, Trinidad.

15, ARCA FILICATA, spec. Nov.

Shell subquadrate, oblique, somewhat inequilateral, rather inequi-
valve, with about thirty ribs, broader than their interstices, and
nodosely crenate, becoming nearly smooth on the disk of the right
valve ; beaks prominent, oblique, their apices rather remotely sepa-
rated by a broad and well-developed lanceolate ligamental area;
_ Imargins strongly dentate, rounded, forming angles anteriorly and
posteriorly with the hinge-line, which is straight, and furnished with
a regular series of small parallel teeth.

A species allied to A. pexata, but having the umbones separated
by a well-developed ligamental area, which is nearly wanting in
that shell.

Lower Miocene, Manzanilla, Trinidad.

16. GRYPHHA ATHYROIDES, spec. nov.

Shell oval, gibbous, slightly irregular; upper valve convex,
marked by deep and wide sulci of growth; lower valve broadly
carinate along its mesial portion from the umbo to the front mar-
gin, plicated by several obsolete radiating folds; lines of growth
strongly marked, undulated; umbo small, produced, and abruptly
truncate.

This oyster resembles an irregular Brachiopod ; and the umbo of
the lower valve is produced and truncated by a circular concavity
resembling a foramen, but which does not extend into the interior.
The microscopic structure also excludes it from the ues Brachiopoda.

San Fernando beds, Trinidad.

VOL. XXII.—PART I. 2k

584 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (June 20,

17. SprroRBIS CLYMENIOIDES, spec. nov.

Tube coiled, discoidal, compressed; whorls usually three to four,
flattened or even fused together, with sinuo-radiate lines of growth ;
periphery carinate ; aperture constricted, circular; nucleus with an
obsolete aperture nearly as large as the terminal one.

The nearest species to this is S. spirulea, Lam. (Spirulea num-
mularis, Schlot.), from which the present species may be distinguished
in never having the last whorl produced or separated.

San Fernando beds, Trinidad. Specimens frequently occur in
the cherty nodules, containing immense numbers of Orbitoides Man-
tel, Nummulina, Cardita, and the curious fossil next to be de-
seribed.

CIssEIS, nov. gen.

Body small, depressed, unattached, divided into rays; oscula few,
large, generally disposed along the summits of the rays, and sur-
rounded by more numerous pores, which are developed on both
surfaces.

18. CISSEIS ASTERISCUS, Spec. NOV.

Body divided into obtuse, somewhat carinate rays, generally four,
but occasionally more; oscula disposed along the summits of the
rays, and particularly on the subconical apex; pores numerous.

The oscula, or larger apertures, are disposed in a group of seyen
or eight upon the apex, from which a row is continued along the
summit of each ray. The general form of the body is that of a
small Palmipes. Between the rays and towards the margins the
pores become smaller and less distinct.

The nature of this body is so problematical that my object in
describing it is rather to make known its existence, and possibly to
obtain some hint as to its true nature, than to draw any inference
from its occurrence. It is found in considerable numbers among the
Orbitoides and Nummuline at San Fernando, in Trinidad. As it
appears by its structure to be more akin to the fossil sponges than to
any other organisms, I have described it as such, at the same time
giving it a generic name which does not involve any view as to its
true affinities. It may possibly be a Foraminifer ; but the nature of
the pores and the want of division seem to be against that view,
and the same characters appear to preclude our placing it with the
Echinodermata. In all the specimens I have examined the pores are
filled with a mineral infiltration, in a similar manner to those of the
Orbitoides. The structure is perhaps as near to that of Sparsispon-
gua as to that of any other organism.

III. OsseRvaTIoNs ON THE RELATIONS OF THE CARIBEAN MI0CENE
Fauna.

From the researches which have been made into West-Indian
Paleontology it appears that the fauna of the Miocene period in
these islands presents some marked distinctions from that of the
United States, and had a stronger resemblance in several of its
leading characters to that of Europe,—not that there were no species

>

1866. | GUPPY—-WESTI-INDIAN TERTIARIES. 585

common to the Miocene of the West Indies and that of North
America, but that those types which give a distinctive character to
the fauna of the Caribean Miocene, and which assimilate it to that
of Europe, were absent from the North American province. When
to this is added the likeness of the Miocene faunas of the West
Indies and of Europe to that now existing in the east, it becomes
a matter of high interest to explain the causes of that simi-
larity, especially as it has been urged of late that a similarity of
organic contents implies a want of contemporaneity in the contain-
ing -deposits when separated by a considerable interval in space.
Such explanation may possibly be found in the former distribution
of land and water allowing or preventing the free migration of
organic beings.

Respecting the Atlantis hypothesis, it is unnecessary to suppose
that the Atlantis existed as a continent up to the close of the Miocene
period. It appears just as easy to account for the facts by suppo-
sing the existence of such a connexion antecedently to the Miocene
period* ; for, as far as regards the Swiss flora, Heer does not consider
any of the species to be identical with living or fossil American forms.
If they are merely closely allied species, they may have been derived
from common ancestors in the Eocene period, or, at any rate, in the
beginning of the Miocene. Our views on this point must partly
- depend on the longevity of vegetable species as compared with those
of Mollusca; but, as bearing on the subject, we have the testimony
of Lesquereux and Newberry that the Eocene plants of America are
closely related to those of the Miocene of Europe, as well as to the
recent flora of the former country; ; and American geologists seem
to entertain no doubt as to the Eocene age of these remains, the
deposits in which they are imbedded having been proved to pass
under the Claiborne (Kocene) beds.

I see, then, some ground for adhering to the views entertained by
Forbes and Godwin-Austen, concurred in by Darwin, and supported
by Dr. Duncan’s investigations, that Europe was probably during
the Miocene period. much in the condition of the present Pacific
Ocean, and that, as observed by the latter paleontologist, it is
reasonable to infer the prolongation of the maze of islands across
the Atlantic. The Mollusca of the Caribean Miocene generally
betoken a clear sea, and probably lived on the slopes of coral-banks.
As confirmatory of this view, I may cite the absence of littoral shells
from the Caribean Miocene fauna.

When the climate of Europe became inimical to the existence of
those species which were adapted only to a high temperature, they
would migrate or become extinct; and supposing that the Atlantis
had in the meantime become broken up and submerged, their migra-
tion would take place towards the east, presuming that there was a
sea-passage in that direction, which seems to be generally considered

* Vide Intellectual Observer, No. lvi. pp. 88-97. Mr. Jenkins informs me
that his paper was written in ignorance of the coincidence in the views we enter-
tain on this subject, and without a knowledge of the contents of this paper,

+ Dana, ‘Manual of Geology,’ p. 513.

2R2

556 * PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

extremely probable. It would also render the paleontological facts
more easy of explanation if it could be shown that the breaking-up
and submergence of the Atlantic land began in the west and pro-
ceeded towards the east. From such a succession of circumstances
it would result that, while the European Miocene fauna would be
related to the Eastern recent fauna, the relations of the Caribean
Miocene fauna would be towards the European Miocene and the
Eastern recent faunas, which seems to be in conformity with the
facts already set forth, as I shall further endeavour to show in this
paper. The affinities with the Eastern fauna are, as might be ex-
pected, somewhat less close than with the European Miocene.

The inferences arrived at from a study of the Asiatic recent and
Tertiary faunas gives support to the view that the migration of ©
organized beings was towards the east, and not from the east. Mr.
Jenkins, in his paper on Javan fossils, has ably summed up the
arguments on this head*; and it is obvious that if Miocene forms
migrated from Europe to the East Indies, where they are in part
still living, they could hardly get across the Isthmus of Panama in
time to be imbedded in Miocene deposits, unless the latter could be
shown to be equivalent in time to the later Tertiaries of Europe
(Pliocene), which, considering the great change in the fauna since
the deposition of the Caribean Miocene, a change indicated by the
extinction of 80 per. cent. of the Mollusca, can hardly be assumed on
such grounds,

I shall now consider more particularly the tendency of the testi-
mony furnished by the fossils. And, taking first Cytherea planivieta,
of the Miocene of Jamaica, it is to be observed that this fossil has
no near recent ally in the West Indies, but it is closely related to
C. erycinoides of the Miocene of Europe. Now both C. erycinoides
and C. planivieta are closely related to C. erycina of Ceylon. As it
is a physical impossibility that a migration should take place from
the existing to a fossil faunat, it follows that the Miocene form
must have migrated to the east. But as the West-Indian shell is
allied to the Bordeaux species, it may have been that its route lay
through southern Europe, which it possibly reached through north-
ern Africa. Its West-Indian Miocene form was thus C. planivieta,
its European Miocene form C. erycinoides, and its Eastern form C.
erycina. Lest it should be supposed, however, that I rest my case
on a single species, I will mention some other examples. Taking the
Echinoderms first, we find that three species of Hchinolampas occur
in the Caribean Miocene, their nearest allies being found in the
Maltese beds. That genus is quite extinct in the West Indies, its
place being filled by Echinometra, which is as abundant now amongst
the Antilles as the extinct Echinolampades were formerly. The only
recent species of Echinolampas, three in number, inhabit Senegal,
the Red Sea, and the Pacific. Cidaris Melitensis, of Anguilla, is to
me undistinguishable from the Maltese urchin. Of the genus
Cidaris the living species are chiefly found in Eastern seas.

* Quart. Journ. Geol. Soc. vol. xx. (1864) p. 62.

+ Hamilton, Address to the Geol. Soc., Quart. Journ. Geol. Soe. vol. xxi. p xciy.

1866. | GUPPY—WEST-INDIAN TERTIARIES. 587

Schizaster Scille is another species common to the Miocene of
Anguilla and the Maltese beds. No recent species are known of
Schizaster in the West Indies, the only species so described (Peri -
aster Cubensis) being really a fossil from Cuba and Guadeloupe.
The present distribution of the six recent species, including two
Periasters, is North Europe, Mediterranean, Red Sea, and Australia.
These three genera are plentifully represented in the European
Miocene. A mollusk of strongly marked type, which has analogous
relations, is Tellina biplicata, found fossil in North America, in San
Domingo, and Cuba, and in the Caroni series of Trinidad. It is
closely allied to 7’. Sobralensis of the Portuguese Tertiaries, and to 7’.
ephippium of the Indian seas. Among the extinct forms we find
many relationships of this sort; but in all the cases here cited the
affinity is most decided; and I have confined myself to those where
the indicated alliances of the fossils are much more close than to any
existing West-Indian forms, and I have avoided genera such as
Natica, Turritella, Pecten, Murex, &c., where the affinities of dif-
ferent species are so various and complex as to render comparisons
somewhat doubtful. But I will now consider the bearing, which is
scarcely less remarkable, of some of those still-existing species of
Mollusca which have been found in the Caribean Miocene. The
most noticeable of these are Bulla striata, Iucina Pennsylvanica, and
L. tigrina. The two former, which occur in the European Miocene,
have not, I believe, been found in the Eastern seas, nor do they —
exist on the west coast of America. Had they not been discovered
in the Caribean Miocene, their existence in the West-Indian seas
might have been cited to show that species from the European Mid-
tertiary fauna had migrated to the West Indies, whereas now that
they are found to occur in the Miocene of the West Indies such an
inference becomes more doubtful. Lucina tigrina is so well-known
and so well-marked a species that its distribution is of some interest
here. We find that this species, fossil in the Miocene of San |
Domingo and of Europe, is now found living in the West Indies, at
Senegal, in the Red Sea, the Mozambique. Channel, and the Indian
seas, and it also occurs fossil in Egypt*. It does not occur on the
west coast of America. But in order to avoid the inevitable length
to which this paper would run were I to attempt to enumerate all
the cases of this kind, I have appended a table in which a few of the
most striking of these affinities are displayed. I will therefore con-
clude this part of the subject by mentioning two more instances—
that of the genus Cassidaria, which is represented by two species in
the Caribean Miocene, but confined in the living state to the Medi-
terranean, and that of the genus Malea, which, like Cassidaria, has
species in the Miocene of Europe, but its living species occur in the
Eastern seas, none being known from the West Indies.

* Deshayes, Conchyliologie, vol. i. pt. 2. p. 795.

588 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

IV. Tasie sHOWING THE AFFINITIES, OF SOME OF THE FossILs OF THE
CaRIBEAN MIocENnE.

a. Species still living.

European Miocene. Living in
Nassa inecrassata ......... N. incrassata. Mediterranean.
Dritonyeemmiatws|.ey.! ee. -pe tenes eee Philippines, &c.
Pyrula melongena ...... P. melongena. West Indies.
Bulla striata ............... B. striata. West Indies.
Venus Paphia ............ V. Paphia West Indies.
PUCKPELA Fi osc) meee eee eet ace Indian Ocean.

Lucina Pennsylvanica...) L. Pennsylvanica.| West Indies.
West Indies, Red Sea, Senegal,
Mozambique, Indian Seas.
Ostrea Virginica ......... O. Virginica. North America.

[TOMA Warnes tates ee L. tigrina.

b. Hatinet Species.

European Miocene analogue. Living analogue.
Cassis monilifera.......... C. diadema.
Cassidariaysulblasvigatan a! (ates sexe. tice aseeauetae ns C. striata. Mediterranean.
Oniscia Domingensis ...| O. cithara. s O.cancellata, Madagascar &e.
Persona simililinna, a.cs.|; saecna scenery ce ebst assets P. clathrata. Madagascar &e.
Myphas alatis) cise... T. affinis, Lichw. T. pinnatus. Eastern Seas.
Mitra Henekeni ........| M.scrobiculata, Broccht. | M. filosa. Eastern Seas.
Ficula carbasea............ F. clathrata, Lam. F. reticulata. Eastern Seas.
Columbella gradata...... C. curta, Bell.
Cytherea planivieta ...... C. erycinoides. C.erycina. Ceylon.
Tellina biplicata ......... T. Sobralensis, Sharpe. | T.ephippium. Indian Ocean.
Pecten Mortomt %./satmen|bs spina: eo tee de eaceora ane P. Japonicus. Japan.
Cidaris Melitensis......... C. Melitensis.
Clypeaster elllptictisen hiv ce cecbe deme sehaatealceh tele C. Australasia. Eastern Seas.
Echinolampas semiorbis | E. hemisphericus. Livi ‘ia NCTE
lycopersicus......... E. scutiformis. ee SOOO ee
Schizaster Scille ......... S. Scilla. ae
Fasciolaria Tarbelliana | F. Tarbelliana, Graz. F. filamentosa. Ceylon &c.
Cancellaria Moorei ...... C. ampullacea, Brocchi. .

The tendency of all these facts can hardly be mistaken, and I
think I have said enough to show that my conclusions are based on
no mere superficial analogy. JI have endeavoured to suggest what
seems the most probable explanation ; and I may add that, as it has
been shown that it is highly probable that a great part of North
Africa was submerged within the Tertiary period*, it may be that a
part of the West-Indian Miocene fauna migrated to south Europe
and the East by that route. As I have already mentioned, Lucina
tigrina occurs fossil in Egypt. It will be unnecessary for me to say
more on this point, because it is easier to explain the migration of
species on this side of the Atlantic than to account for the mode in
which they crossed that ocean. It is not, however, without some

* See Martins, Rev. des deux Mondes, July 1864, cited in the President’s
Address, Quart, Journ, Geol. Soc. vol. xxi. p. lxxxiii.

1866. ] GUPPY—WEST-INDIAN TERTIARIES. 989

significance for this view that the corals of the Miocene beds of
Madeira are analogous to those existing in the Red Sea*.

The arguments which have induced me to favour the view that
there was some former connexion between the shores of the Atlantic,
do not entirely forbid the supposition that there may have been,
during some part of the Tertiary period, a connexion, by the way of
~Panama, between the Atlantic and the Pacific. Mr. G. H. Saunders
discovered fossils of the Caribean Miocene on the isthmus in a cut-
ting of the Panama Railway?y. Mr. Carrick Moore has given us a
list of West-Indian Miocene species related to Pacific formst, all of
which, however, do not occur on the coast of America. There is also
a certain relationship between the recent faunas of the two sides of
the isthmus, as indicated by the following list of species either
identical or so nearly related as in some cases to present difficulty in
their separation :—

Cytherea Dione, West Indies and Mazatlan.
Purpura patula, West Indies and Panama.
Modiola Braziliensis, Ff ~
e Mactra similis, ‘
Purpura undata, West Indies = P. piserialis, Panama.

Sp., » » =P.nodosa, __,,
Area illota, # » = A.Tayboyensis, ,,
Adamsi, = 3 = Avsolida; Gs

This is not intended as an exhaustive list; but it is obvious
that there is nothing in it that would lead us to assume anything
more than a very partial migration. We do not find here that
strong chain of affinities which leads us from the Caribean through
the European Miocene to the shores of Madagascar and Ceylon. We
find, indeed, that those typical forms which are common to the
Caribean Miocene and the Indian seas do not occur on the west
coast of America.

The general conclusions at which I have arrived may be shortly
stated as follows :—

1. That the distribution of fossil and recent species shows it to be
highly improbable that the West-Indian Miocene forms reached the
localities where they occur as fossils by way of the Isthmus of Pa-
nama, or by an easterly route from Europe or from the Indian seas.

2. That it is probable that there was during the early and middle
Tertiaries such a connexion between the shores of the Atlantic as
admitted of the migration of organized beings from one side to the
other, although the continents may not have been absolutely joined.

In regard to the latter of these conclusions, it seems that the
evidence before us can scarcely yet justify any positive assumption
- as to the particular direction in which the migration of species took
place, or whether the origin of the typical forms of the Miocene was
on the western or the eastern side of the Atlantic, or in the interme-
diate region. Another view is that there might have been an inter-
change of species; but this would require a closer and more perma-

* Lyell, ‘Elements of Geology, 6th ed. p. 668.

+ Quart. Journ. Geol. Soe. vol. ix. p. 132.
t Lbed. vol. ix. p. 131.

590 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

nent connexion of the two sides of the Atlantic. On the whole, the
balance of evidence appears to be in favour of the view that there
was migration from the western to the eastern side of the Atlantic.

In conclusion, I may observe that I have been unavoidably led to
support a modification of the Atlantis hypothesis provisionally, and
until it can be clearly shown what theory can best reconcile the
facts. It is to be hoped that our information relating to the Tertiary
formations will be increased by all who have it in their power to do
so; for principles may thus be made manifest which may hereafter
be applied to the study of the older formations. I readily admit
that I have by no means exhausted the analogies of the fossils treated
of in this paper. I fully believe that more relations will be esta-
blished between the fossil faunas of San Domingo and Jamaica and
Europe and the living fauna of the Indian seas than I have been
able to determine satisfactorily. Iam aware of the shortcomings of
my papers in this and other respects ; but I trust that others may be
induced to carry out still further the comparisons I have attempted,
and to show thcir real import. It may be that I have fallen into
some errors; but I hope that the true inferences may be drawh from
the facts. I believe that one of those inferences will be, that the
Miocene of the West Indies must be included in the same great
period of time as that of Europe, and may therefore be considered,
in a geological sense, synchronous—though even in this instanee the
doctrine of homotaxis may be so far true that neither the commence-
ment nor the termination of the Miocene period, as indicated by
organic types and limited by physical changes, may have been
simultaneous in the European and Caribean areas.

EXPLANATION OF PLATE XXVI.
(Illustrative of West-Indian Tertiary Fossils.)
[The figures are all of the natural size, with the exception of fig. 19 a.]

Fig. 1. Cercomya ledeformis. Manzanilla, Trinidad.
2. Mactrinula macescens: 2a, hinge of left valve; 26, hinge of
right valve; 2c, exterior of left valve. Manzanilla, Trinidad.
3. Arca Trinitaria: 3a, posterior view of the shell with the valves
united; 3, exterior of left valve. Manzanilla, Trinidad.
4. Cardium castum. Manzanilla, Trinidad.
5. Arca filicata. Manzanilla, Trinidad.
6. Erycina tensa. Manzanilla, Trinidad.
7. Ficula carbasea. Savanetta, Trinidad.
8. Corbula vieta. Manzanilla, Trinidad.
9, Ancillaria lamellata. Manzanilla, Trinidad.
10. Sptrorbis clymenioides. San Fernando, Trinidad.
11. Nassa solidula. Cumana.
12. Turritella tornata. Cumana.
13. Cytherea guncea. Cumana.
14. Melanopsis cepula. Cumana.
15. Dosinia cyclica: 15a, exterior of right valve; 150, hinge of
’ right valve. Manzanilla, Trinidad.
16. Venus Wall. Manzanilla, Trinidad..
17. Gryphea athyroides. San Fer nando, Trinidad.
18. Ranina porifera. San Fernando, Trinidad.
19. Cissets asteriscus: 19a, portion magnified; 194, the whole of
the fossil, natural size. San Fernando, Trinidad.

7 ~~

Quart.«J ourn Geol. Soc Vol XXI1L-P1 XXXVI.

2 6

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Wee ei AN TERTIARY FOSSibS

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1866. | WOODWARD—NEW SPECIES OF RANINA. 591

Nore on a Nuw Specrus of Rantna (R. porifera) from the Textrary
Srrata of Trinmpap. By Henry Woopwarp, F.G.S., F.Z.8.

A specimen of a Crustacean placed in my hands for examination by
my friend Mr. R. Lechmere Guppy, from the Tertiary formation of
Trinidad, proves to be a portion of the dorsal surface of the carapace
of a Brachyurous Decapod—nearly approaching the Anomuwra—
belonging to the subsection Motopoda and the genus Ranina.

The species of this genus (which was established by Lamarck in
1801) are not only most singular in form, but they are of special
interest to the paleontologist as occurring in the Nummulitic Lime-
stone of Bavaria, Austria and Italy, Asia Minor, Scinde, and the
West Indies (Trinidad), and also in the Oligocene of Germany and
the Miocene of Turin. Nor hasthe genus now disappeared; for at
the present day itis represented by the Ranina dentata of Latreille,
which is found living in the Sandwich Islands, the Moluccas, the
Mauritius, and Japan (De Haan, Siebold’s ‘ Fauna Japonica,’ 1833,
p. 139, t. 34 & 35), whilst a nearly allied genus, the Raninoides,
Edw., is found living in the Philippine Islands and Trinidad, having
been collected in this latter locality by Mr. Guppy.

The following is the list of all the species known to the author :—

Ranina

1. Aldrovandi, Ranz (Mem. di Storia nat. Dec. 1, 1820, p. 73, t. 5).
Lower Eocene Nummulitic formation. Kressenberg, Valdenega, and
Madugi d’Auzago.
. Tchihatcheffi, d Arch. (Progr. de la Géol. iii. p. 303).
Nummulitic formation. Asia Minor.
. Marestiana, Konig (p. 20, taf. 5. fig. 1, 2).
Nummulitic formation. Kressenberg and environs of Verona.
. Haszlinskyi, Reuss (Foss. Krabben, p. 22, t. 4. f. 4, 5).
Upper Eocene? LEperies, Hungary.
. speciosa, Minster, sp. (Miunst. Beit. zur Petrefact. iii. p. 24, t. 2. f. 1-3).
Oligocene. Binde.
. oblonga, Minster, sp. (7. c. p. 24, t. 2. f. 4).
Oligocene. Ebenda.
. palmea, Sismonda (Acad. Leop. Crost. Foss. Piemonte, t. 3. f. 1).
Miocene. Colle di Torino.
. sp. (Reuss, Foss. Krabben, p. 21, t. 5. f. 3, 4).
Nummulitic. Environs of Vicenza.
sp. Nummulitic formation. Kurachee, Scinde. Collected by Major
W. E. Baker. (In British Museum.)
. porifera, H.W. Tertiary. Trinidad. R. L. Guppy, Esq.
. dentata, Latr. (De Haan, ‘ Fauna Japonica, 1833, p. 189, t. 34 & & 35).
Living. Japan, &e,

HO 0 ON OD oO FP & DW

et

The Ranine are all burrowing forms of Crustacea, living for the
most part in deep water, buried in sand or mud, for digging in
which their limbs are most admirably adapted.

Unfortunately none of the appendages are preserved in the speci-
men under consideration ; but all the species of this genus are curi-
- ously sculptured upon the dorsal surface of their carapaces, and this
ornamentation is extremely characteristic of the group. It consists
of irregular transverse pectinated ridges, sometimes interspersed with
small punctations, the ridges being more or less curved and interca-
lating with one another.

592 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

In Prof. Reuss’s work (Foss. Krabben der k.-k. Akad. der Wissen-
schaften, Wien) these peculiarities are very well shown; but neither
in these nor in the various specimens which I have been able to
examine can I detect the same ornamentation as that observable
in the Ranina from Trinidad.

Each minute point forming the pectinated border to the several
ridges has a small indented pit near its extremity, which has sug-
gested the specific name porifera (see Plate XXVI. fig. 18). It is
to be hoped, however, that more perfect specimens will reward the
zealous labours of Mr. Guppy, as the determination of species upon
the evidence of a single fragment, offering such meagre characters
as the one now noticed, is by no means safe, except in very peculiar
and well-marked forms, such as the species of the genus Ranina.

With regard to the species nos. 8 and 9 in my list, I am inclined
to consider that figured by Prof. Reuss from the Nummulhtie forma-
tion of Vicenza and the specimens brought over by Major Baker from
Scinde (and now preserved in the British Museum) to be identical.

The pectination is coarser and stronger than in Ranina porifera,
and there are no indented pits at the extremities of the teeth form-
ing the transverse serrations on the surface of the carapace.

I beg, therefore, to propose for these specimens the specific name
of Ranina Reussv, in honour of the distinguished Austrian palzeon-
tologist who has figured it in his work.

Note on the OrsirorpEes and Nummvuin»® of the Tertiary AsPHALTIC
Bep, Trinipap. By Professor T. Rupert Jonus, F.G.S.

Tue asphaltic rock yielding Orbitoides and Nummuline in abundance
is described in the ‘ Report on the Geology of Trinidad’ (1860,
p- 87), by Messrs. Wall and Sawkins, as a highly inclined bed of
bituminous shelly marl, protruding on the coast at San Fernando,
on the west side of the island, and forming part of the “ Naripima
Marl,” in the “ Newer Parian Group,” regarded as being probably
Miocene, whilst the “ Older Parian,” on which it rests, is Neocomian
in age. |

In 1863 Mr. R. L. Guppy read a paper descriptive of this peculiar
stratum before the “ Scientific Association ” in Trinidad, pointing out
that its shelly contents are Orbitoides and Nummulites, the former
predominating; and he suggested that in all probability they would
be found to be of the same species as those referred to in my ‘‘ Note
on the Nummuline and Orbitoides of Jamaica” (Quart. Journ. Geol.
Soc. vol. xix. p. 514). This opinion is confirmed by a careful
examination of specimens of the asphaltic. stratum, with which ~
Mr. Guppy has favoured me.

Boiled several times in turpentine, this rock loses its bitumen,
and resolves itself into loose Orbitoides and Nummuline, with a few
other Foraminifera, and (when cleaned by acid) a small proportion
of green-black sand and very few rounded grains of quartz. On the
weathered surfaces of the rock, and in pieces carefully burnt, many
perfect Orbitoides may be recognized; and probably throughout the

1866. ] NEALE—-GOLD IN ECUADOR. 593

mass the specimens are mostly well preserved; but it is difficult to
get them out whole and clean, except by long steeping in hot
turpentine, changed from time to time. The Nummuline keep
‘rather more perfect in the process of cleaning. The many aspects,
however, of the broken specimens enable us to determine their
‘relationships without the trouble of grinding and polishing. When
the asphalt is driven off by heat, the Nummulites often fall into two
pieces by splitting along their median line of chambers; but this
horizontal section is not generally so useful in determining species
as the exposure of the successive surface-layers. __

The majority of the Orbitoides, mainly constituting this rock, are
small and biconvex, with somewhat expanded edges, about + inch
broad and 54, inch thick at the centre. There are also occasional
evidences of broader, thin Orbitowdes. The Nummuline, not nearly
so numerous, are smaller still; biconvex, with a sharpish edge, and
_ measuring about ;, by 4, inch. A fragment of a small Nodo-
saria raphanus and a Discorbina also occurred to me, together with
a piece of a little Echinoderm-spine*.

The Orbitoides is exactly the same as the variety from the Tertiary
sand of Orakei Bay, New Zealand, described and figured by Karrer,
in the ‘ Novara Expedition’ (Geol. Theil, I. Band, 2. Abtheil. Pa-
leont. p. 86, pl. 16. fig. 21), as O. Orakeiensis, Karrer, which,
there is reason to believe, is a variety of O. Mantelli, Morton, a spe-
cies found in America, the West Indies, and Sinde (see Geol. Mag.
vol. 1. p. 75, and p. 103). The Nummulite is one of the small
“‘ sinuo-radiate” varieties (sometimes simply “ radiate”), such as
are referred to by me in the note on the Jamaican Nummuline, and
in the ‘Geol. Mag.’ loc. cit., as present in the West Indies, Sinde,
and Kurope (Vienna) in rocks probably of Middle Tertiary age. It
may be catalogued as N. Ramondi, Defr. (=. radiata, D’Orb.),
which is found associated with Orbitocdes in Jamaica, Antigua,
and Sinde.

a

8. On the Discovery of new Goxrp-pEposits in the District of Esmx-
RALDAS, Ecuapor. By Lieut.-Col. Epwarp Sr. Joun Neate, H.M.
Chargé d’Affaires in Ecuador. Communicated by the Secretary
of State for Foreign Affairs.

Wirnin the last few weeks+ unworked and hitherto unknown
gold-deposits have been discovered in the district of Esmeraldas ; and
I am informed by the President, who has received specimens of the
gold of a very pure quality, that it is the intention of the Govern-
ment to send a scientific Commission, at the head of which will be
Dr. Jameson, a British subject who has been many years in Quito,
to report upon the probable yield of the gold-district.

* Mr. Guppy believes he saw Polyzoan remains in this band; but possibly
detached pieces of the cellular superficial layers of the Orditoides, much resem-
bling Cellepora &c., may be the forms alluded to.

1 This communication was dated April 18th, 1866.

594 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

Should this survey prove satisfactory, as anticipated, I am im-
formed that the Government of this Republic will be prepared to
enter into engagements with foreign speculators and capitalists.

9. On Bonzs of Fosstz Cuetonrans from the OsstrErous Caves and
Fissures of Matra. By A. Lerra Apams, M.B., F.G.8., Surgeon,
H.M. 22nd Regiment.

Rematns of more than one species of River-tortoises have turned
up occasionally in the Maltese caves and fissures of the downcast and
denuded districts, in localities situated from three to six miles
and a half apart, and always associated with remains of the fossil
Elephant, Hippopotamus Pentland:, Myoxus Meltensis, and Birds—
the last, chiefly aquatic, including the Cygnus Falconert of Parker,
besides a Lacerta, of about the dimensions of the common Chameleon,
and one or more Frogs. The nature and arrangement of the deposits
and conditions of this fossil fauna clearly show that all the remains |
had for the most part been conveyed into the above situations by the
agency of largebodies of water which at one time overflowed the greater
portion of the eastern half of Malta. None of the Chelonian bones ex-
amined by me give indications of the presence of either land or marine
species, but agree in their characters with the Hlodians and Pota-
mians. The largest comprise part of the right and left femurs of
perhaps the same individual, a detached lower extremity of a
humerus, several tibize, and one cervical vertebra from Mnaidra
Gap, besides a large caudal vertebra from Benghisa Gap, which is
six miles distant from the former, and situated at the extreme south-
east point of the island. Among organic remains from the Zebbug
Cave, in the middle of the island, I also observed fragments of bones
of individuals equal to, if not somewhat larger than, any here de-
scribed ; also a portion of a humerus of a species of very much smaller
size. A glance at the femurs above mentioned shows, by their oblong
heads and the trochanters being separated by a deep and arched de-
pression, that they belonged to either a Marsh- or River-tortoise.
Their dimensions are as follows :—

Transverse measurement from head to trochanters... 3°5 inches.

Antero-posterior length of tuberosities.................+6 2G yee
Lengthyof head 7 saso5 A ce aestnne tases deca coe renee rine Th We
Breadth of head: (5.5.26S heck sans Oeasee os costen cece eee eee Oe
Garth ol heads vaca ices awonooncstln Gavin ee eeRE Cees GD
Garton necks. 08 Sse Ne ee ae de ee GO: 32
Depth of intertrochanter notch ............c..cceeeseeeees 3 lines
Girth of shaft, three inches below the trochanters...... 4-5 inches.

thus representing an individual nearly four times as large as the
Chelys matamata, and about two feet in height. A tibia entire, but
belonging to a smaller individual than the last, is 3-6 inches in
length, with a girth of 2 inches in the middle; whilst that of its
proximal end is 4-5 inches, and the distal 3-5 inches. Another tibia,
which has lost its lower extremity and part of the shaft, retains 4°5
inches of the upper portion ; the circumference of the head is 5-3

He66;) °° LEITH ADAMS —HALITHERIUM. 595

inches, and of the middle of the shaft 2-5 inches. The lower extre-
mity of a humerus is 2°3 inches across the articulation ; the furrow
on the external border is faint, which, again, distinguishes the bones
in question from those of marine turtles.

A cervical vertebra, possibly the 5th or 6th, has lost its anterior
half; but the convex end and vertebral foramen, together with the
articulating processes, are entire. The breadth of the convex arti-
culating surface of the body is 1-4 inch, by 1 inch in thickness;
entire height of the vertebra 2°2 inches. The caudal vertebra from
Benghisa Gap has also lost its posterior portion ; and transverse pro-
cesses of the body, with the concave articulation, canal, and anterior
superior articulating facets, are preserved. The concave articulation
is 0-9 inch broad by 0°7 in the antero-posterior direction; the
height of the vertebra 1-7 inch, and diameter of the canal 0:3
inch.

A humerus of a very small species of Tortoise from the débris of
Zebbug Cave shows only the head and a portion of the shaft, the
curved condition of the latter clearly distinguishing it from the
Marine, whilst the greater comparative width between the tuberosi-
ties separates it from the Land, and assimilates it to either the Marsh
or River families. ‘The fragment measures from the head to the
tuberosities 5:5 lines; distance from one tuberosity to the other 5
lines. The head is 3°5 lines vertically, and 3 lines broad; girth of
shaft 3 lines.

10. On the Discovery of Rematns of HatirnErium im the Miocune
Deposits of Matta. By A. Lerra Apams, M.B., F.G.S., Surgeon,
H.M. 22nd Regiment.

Various forms of Cetacea have been met with in the four upper
beds of the Miocene strata of the Maltese group. The discovery there
of teeth of Zeuglodon by Scilla, and the abundant remains of one or
more species of Dugong allied to recent forms
and Balen, show the prevalence of these
mammals in the seas of the period. They
are met with in the greatest numbers in the
sand-bed and nodule-bands of the Calca-
reous Sandstone. In the latter situation I
lately discovered a tooth which appeared to
me to belong to the Halitherium, and in the
sand-bed an ear-bone and caudal vertebre
of possibly the same genus. The tooth and
ear-bone I have shown to Professor Owen, who has confirmed their
identity with the above-named genus.

The molar, possibly a penultimate, has lost one of its fangs.
The crown is encased in thick shining enamel, and is 9 lines in
length by 8 linesin breadth; the height of the crown is 2:6 lines.
The fangs are two in number; the anterior small, the posterior large
and diverging. The length of the latter is 7:5 lines.

Tooth of Halitherium.

596 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

The accompanying sketch represents the crown (nat. size), which
probably shows a more advanced state of wear than any figured by
Cuvier*.

The ear-bone is entire, and measures 1-4 inch in breadth, by
9 lines in vertical diameter.

The specimens referred to in this note are in the Museum of the
Geological Society. te he

11. On the Arrinirius of CHonpRostzvs, Ag.
By Joun Youne, M.D., F.G.S.
(This paper was withdrawn by permission of the Council.)

[ Abstract. 1]
TE object of this communication was to show, from the characters of
the skeleton, that Chondrosteus belongs not to the Chondrostean
division of the ganoids as. stated by Agassiz, but to the Holostean
division, since it possesses a well-ossified basioccipital; and the
lateral walls of the cranium are composed of bones answering to the
cartilage bones of ordinary Teleosteans.

12. Notice of New Grnnra of CaRrBonirERous GLYPTODIPTERINES.
By Joun Youne, M.D., F.G.S8.

Styce the publication, in 1861, of Professor Huxley’s memoir on
the classification of Devonian Fishes, several new genera have been
established, and the intervals between some of the families (tabu-
lated at p. 24, Mem. Geol. Surv., Decade x.) thereby diminished.

- Rarzoporsis, Huxley. Fig. 8.

The specimens to which this generic name has been given are
those whose scales Prof. Williamson described and figured in the
Phil. Trans. 1849, under the name of Holoptychius sawroides, a
term which has also been applied to a tooth which it will appear is
generically distinct from Holoptychius.

The body of this fish tapers to a point posteriorly; its greatest
depth is at the pectoral arch. Head depressed; orbits forward;
gape wide, extending behind them. Maxilla in a single piece, fur-
nished with fine, equal, conical teeth; premaxilla not preserved.
Mandible straight, deepest posteriorly, expanded at the symphysis ;
contains teeth of two sizes; the larger, three or four in number,
plicate at the base, strong, conical, slightly incurved; the smaller,
one-fourth of the size of the preceding, like them strong, conical:
the surface of all the teeth above the plicate base is smooth. Jugu-
lar plates in two pairs, principal and posterior. No trace of median
or lateral plates. The occipital region is closed in by three bones,
in front of which are the parietals in close approximation. The
facial bones are not determinable. Operculars large, subquadrate ;
suboperculars a half smaller, rounded anteriorly. The parietals,
operculars, and jugulars are ornamented with fine, parallel or bifur-
cating ridges. The facial bones and jaws have their surfaces reticu-

* Ossemen Fossiles, pl. xxxviii. figs. 9, 10, & 11.

1866. | YOUNG——CARBONIFEROUS GLYPTODIPLERINES. 597

lated by similar anastomosing ridges. The pectoral arch is well
developed, and supports a subacutely lobate fin with rounded margin.
The two dorsals, the ventrals, and anal are of nearly equal size, and
opposite each other respectively. The tail is heterocercal and
rhomboidal.

Figs. 1-8.—Jilustrating the teeth and scales of some new genera of
Carboniferous Fishes.

Pilg
Nt i }
We S ; =;

8 7 6
Fig. 1. Rhomboptychius, tooth. | Fig. 5. Rhizodus, tooth.
2. Rhomboptychius, scale. 6. Megalichthys, scale.
3. Strepsodus, tooth. 7. Dendroptychius, scale.
4. Rhizodus, scale. 8. Rhizodopsis, scale.

The scales vary somewhat in size and shape on different parts of
the body; they are arranged in very oblique series, and range from
nearly orbicular to elongate cordate. The upper surface is orna-
mented with concentric and radiating strie; the latter are most
strongly marked over two triangular areas whose bases correspond
to the centre of the anterior and posterior margins respectively ; the
former occupy the lateral surfaces between those areas. The under
surface is marked by more or less numerous growth-lines, presents
a subcentral raised boss, and is usually pitted over a small area
immediately behind the centre ; no corresponding tubercles are visible
on the upper surface, whose free area averages two-thirds of the
whole surface. The lateral line is well marked and nearly straight.

The notochord is persistent ; the osseous rings surrounding it are
short and narrow. The upper arches are distinct and well ossified.

These characters are in the main those of the family to the cycloidal
section of which Holoptychius belongs. But from that genus Rhz-

598 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

zodopsis is separated by the presence of teeth of two sizes, by the
thinner scales, and by the regularity of the striate ornament over
their whole surface, contrasting with the coarse tuberculation of
the posterior and smoothness of the’ anterior area of the scales in
the Old Red Sandstone genus. From Rhizodus the absence of tren-
chant teeth is a broad distinction; the character of the scale-orna-
ment of the former, as described below, is equally diagnostic.

The specimens which have been selected as typical of the genus
average 5 inches in length. For them the specific name R. sau-
roides has been used, as in Prof. Williamson’s paper, which contains
the only published description in England of the scales. Other
specimens, whose length is estimated at 12 or 15 inches, are imper-
fectly preserved ; it remains to be seen whether they are specifically -
distinct, or whether the greater thickness of their bony scales is
merely a concomitant of the greater size of the fish. The same
doubt exists in the case of the small flexible scales, whose possessors
probably did not exceed 2 inches in length.

In a paper “ Ueber das Vorkommen von Riizodus Hibberti, Owen,
Megalichthys Hibberti, Agassiz and Hibbert, in den Schieferthonen
des Steinkohlengebirges von. Volpersdorf in der Grafschaft Glatz ”
(Zeitschr. deutsch. geol. Gesellsch. p. 272, 1865), Roemer figures
at least one scale presenting distinctly the characters of Rhizodopsis.
The concentric and radial sculpturing is described nearly as above,
with the minor difference that the concentric seem of equal promi-
nence with the radial ridges. But there is some confusion in the
author’s mind—there is at least in his remarks—about the identity
of his specimens with the Scottish genera. For in speaking of the
teeth of Rhizodus he omits notice of their distinctive feature, the
double trenchant edges and the elliptical form of the transverse sec-
tion of the tooth; both are figured (taf. vi. f.5), but only the plicate base
is described. Again, it is said that the thick Scottish scales (which
are not horny, as Roemer says, but osseous) show, when carefully
split off in layers, the same ornament as those which he has figured
as Rhizodus. Admitting the hazard of criticism without sight of the
specimens, I cannot help suspecting that Roemer has fallen into the not
uncommon error of mistaking internal structure for superficial orna-
ment. The suspicion is further strengthened by his statement of
the occasional occurrence of a prominent boss on the outer surface of
his 2hizodus-scales. That such a boss is invariably present on the
under surface is well known; but I have never seen a scale in this
or any other ganoid on which the ornamentation has such astructure
for its centre. Abrasion of the under surfaces of thick scales in which
the boss remains intact while the deeper structure of the scaleis ex-
posed, would give somewhat of the appearance described, and is of
not unfrequent occurrence. But while the presence of Rhizodus,
Owen, in the German coal-strata must be held as unproved, the in-
teresting fact still remains that the genus Rhizodopsis is unquestion-
ably common to the English and German coal-fields : on the identity
of the species it is impossible to form an opinion.

1866. | YOUNG—CARBONIFEROUS GLYPTODIPTERINES. 599

Rutzovus, Owen (=Apepodus, Leidy)*. Figs. 4 & 5.

The teeth of two sizes and trenchant on both edges, on which
this genus is founded, and its distinctness from Holoptychius and
Megalichthys established, are accompanied by scales which are dis-
tinguished from those of the latter genus by the fact that their
anterior area is cycloidal and concentrically striated, not smooth and
rhombic. The free area, on the other hand, is covered with coarse
tubercles, and has a general resemblance to that of Holoptychius.

No fragments have yet been found from which the shape of the
body or the structure of the head can be determined. One or two
varieties of the teeth occur; thus one edge only may be trenchant,
the posterior (?) being evenly rounded. Of such teeth some are
angulated more or less sharply, their section passing from triangular
with rounded angles to polygonal. None of the varieties have been
named, as it is possible that they may be individual differences ;
further, the determination of several teeth hitherto isolated has pro-
ceeded so rapidly that it is better to wait for more materials.

Leidy (Journ. Acad. Nat. Sc. Philadelphia, ii. 1855-58) de-
scribed and figured a tooth of a Carboniferous genus Apepodus, be-
tween which and Rhizodus, as known to British paleontologists, no
substantial difference can be detected. The same beds, said to be of
Carboniferous age, yielded scales which Leidy figures as Holopty-
chius Americanus ; their characters are very similar to those of H.
giganteus, Agassiz (Poiss. Vieux Grés Rouge, pl. 24. f.3-10). Whether
these beds be of Carboniferous age, as affirmed by Leidy, or Upper
Old Red, the association of the two genera in the same deposit is an
interesting fact not yet paralleled in this country.

The scale figured is taken from a large block of limestone from the
Gilmerton quarries near Edinburgh. A similar block is so placedin
the rooms of the Royal Society there as to render its examination a
task of difficulty. The scales are associated, on it, with typical teeth of
Rhizodus, and with fragments of pectoral arches and other portions
of the skeleton. .

The scales are rotundo-quadrate, the anterior margin flattened,
the posterior slightly produced. They are thick, bony; their under ~
surface is marked by concentric growth-lines, and bears a large or
small, but constant, subcentral boss. The overlapped, anterior area
of the upper surface is never less than a moiety of the whole; it is
covered with fine concentric and a few radial strie. The free surface
is thrown into broad undulations, which are approximately parallel

* It is commonly stated that Megalichthys Hibberti is the synonym of Rhi-
zodus Hibberti. Dr. Hibbert’s paper, which is as remarkable for its rare gene-
rosity as for the extent of the research it sums up, contains a passage which shows
that Agassiz had not wholly overlooked the different forms of the teeth, though
he afterwards underrated their importance. Agassiz, it is said, proposed the
name M. falcatus for a form of tooth to be distinguished from that of Burdiehouse
by being very sharp on the edges. Rhizodus is abundant in the Burdiehouse
beds. The assertion, therefore, of a difference as well in locality as form can
only be explained by the rapidity with which the great naturalist passed from
place to place, and thus, while he increased the materials for his scheme of classi-
fication, slipped into minor errors of detail.

VOL. XXII.—PART I. 28

600 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

to the margins of the scale, and about their own breadth apart. The
frequent interruptions of the concentric ridges gives the appearance
of coarse tuberculation, which is increased by the roughened condi-
tion of the summits of the isolated portions. The intervening inter-
spaces frequently show fine radial strie, which may, however, be
those of the deeper, exposed by erosion of the upper layers*.

To the definition of the genus which Owen gave from the form of
the teeth only, M‘Coy, in 1848 (Ann. Nat. Hist,), added the cha-
racters of the scales, which he described as “ thin, rotundo-quadrate,
with smooth under surface, and subcentral boss.” If by “thin,” in
another place “rather thin,” any marked difference is implied be-
tween Holoptychius and Rhizodus, the examples of the latter on
which the present article is founded do not confirm the implication.
Thin scales there are of the form stated by M‘Coy ; but they never at-
tain the dimensions of the larger number of Rhizodus-scales. They
are those of Rhizodopsis, whose superficial ornament is, further, very
different. Portions of scales, one or more lamin of scales, are of not
uncommon occurrence ; and these, perhaps, have suggested the above
generic character. But the probability that M‘Coy has mixed up
two genera, not then recognized as distinct, is increased by the or-
nament ascribed to R. Hibberti (Pal. Fossil. p.612), viz. “ close ver-
micular” ridges. Assuming that these ridges are in reality super-
ficial, and not portions of the deeper structure, there are only two
Carboniferous genera (to be described hereafter) whose scales
are of equal size, and present an approach to this kind of sculp-
ture. They are Dendroptychius and Rhomboptychius. But in the
former the close-set ridges are subordinate to more distant larger
ones, in the latter they traverse conspicuous concentric grooves.
The specimens of Rhizodus which have occurred to me show as great a
variety in point of thickness as those of Holoptychius, e. g. H. Andersom
and H. giganteus. This difference of size may be specific ; but species
can scarcely be founded on isolated scales showing only their under sur-
face. The examples which revealed their upper aspect were as thick
as those of H. giganteus, and, besides the undulating (not tuberculo-
linear) sculpture, had the anterior area also striated (not smooth),
differences which seem to be generic as between the Carboniferous
and Old Red fishes.

The surface of the pectoral arch and dentary bones is covered with
fine tubercles, close-set in small (apparently young) specimens; but.
in the large the tubercles are confluent by their bases, so as to cover
the whole surface with irregular pits or grooves bounded by ridges
of unequal height. A very fine pectoral arch (belonging to the
Natural History Museum, Edinburgh), referred to this genus on
account of the presence of a doubly trenchant tooth, has around it
numerous fragments of fin-rays—long slender tubular rods of very
dense texture, similar to those observed in Dendroptychius.

* The descriptions of Hibbert (Trans. Edin. Roy. Soc. xiii. 24) are unfortu-
nately very meagre ; but there is, I think, reason for believing that the ornament of
Rhizodus, as above described, is intended in the figures of the scales, pl. 10.
figs. 1-3, the specimens floured come from the same beds as those to which I
have referred.

1866. | YOUNG—CARBONIFEROUS GLYPTODIPTERINES. 601

No other portion of the skeleton has as yet been recognized.

Comparison of Williamson’s sections of the scales of a Carboniferous
Holoptychius (loc. cit. fig. 24) with those in the Poiss. Foss. du Vieux
Gres Rouge, further confirms, by the difference of minute structure,
the generic distinctness of the fishes from the two series of rocks.
Further discussion of these microscopic characters is reserved for _
another occasion ; but the vertical section just mentioned, in Wil-
liamson’s paper, is interesting in this, that while the description
corresponds with that of the under surface of Rhizodus-scales, the
form and structure of the upper surface would agree well with that
of a tuberculated scale on which little or no ganoin was developed,
such a scale in fact as I believe that of Rhizodus to have been.
But the point requires further investigation.

Honoprycuivs, Agassiz (excl. Lthizodus)*.

The characters of this genus are summed up in the memoir
already mentioned (p. 5), thus :— :

«‘ Head depressed ; caudal extremity conically tapering, orbits far
forward; gape extends far back, Frontals distinct from one another
and from the parietals, which are large and coadapted, though quite
distinct. The occiput is covered by three bones, a median and two
lateral. There are two principal and a number of lateral jugular
plates, and there is no rhomboidal median plate between the two
principal jugulars. Some of the teeth are larger than the others,
and longitudinally striate at their bases. The paired fins are very
acutely lobate, and there are two dorsal fins in the posterior half of
the body. ‘The ventrals are situated under the first dorsal, and are
succeeded by a single anal. Tail little more than semirhomboidal,
the upper half being much less developed than the lower.”

The diagnosis of this genus from Rhizodus by dentitional charac-
ters and the difference in sculpture of the scales has already been
spoken of.

Dewproprycuius, Huxley. Fig. 7.

The bony scales to which this name was given are characterized
by the division and subdivision of the grooves which traverse their
exposed surface. They are nearly equilateral, with rounded angles.
They vary in size on the same individual; the largest measure about
42ths in length by 1 inch in breadth; but the average is ;/,ths by
_ j;ths. The overlapped area is covered with fine striations, concen-
tric and radial, the latter being most marked over a triangular area
whose base is the centre of the anterior margin. The exposed sur-
face, slightly smaller than that of the preceding, is sharply bounded by
an arcuate line whose convexity looks forward. From this line the
sinuous branching grooves run, those from the centre radially, those
from the lateral parts more directly backwards; they are larger
and fewer in number on the larger scales; their interspaces are
marked with fine anastomosing grooves. The under surface is smooth,

* The scales described under this name by Williamson belong, as has been
already mentioned, to a wholly different genus, Rhizodopsis.
282

602 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

and marked with concentric growth-lines ; a subcentral boss projects
from a shallow depression. The structure of these scales closely
resembles that of Holoptychius.

No teeth are found with them, but many ossified vertebrae with
neural and hemal spines, and the ventral fin-bones and rays.

The best-preserved vertebre are those along with which the
pelvic bones occur. ‘They are longer than broad, slightly constricted
in the middle; their shallow terminal concavities occupy the whole
articular surface, and are perforated by a small notochordal foramen,
whose area is one-seventh of the whole surface. They decrease in
size from before backwards; the anterior having the following ratio

Eength = 777"
Breadth 11°

The neural spines, about 24 inches in length, are mostly seen in
profile; their section is pentagonal, much compressed laterally. At
a short distance from the base, a sight constriction marks off the
articular end, whose convex surface slopes upwards and backwards,
so as to form an angle with the axis of the shaft. The arch in-
cluded between the two lamin is low and wide.

The heemal spines, of nearly equal length with the neural, consist
of a slender tapering shaft, sigmoidally curved, and terminated at
the proximal end by two thin plates triangular in profile and
enclosing between them an arch whose height equals one-fourth of
that of the whole process.

Neither hemal nor neural spines are found in actual contact with
the vertebrae, whose outer surface is removed, so that the nature of
the connexion is not seen. But from being constantly found near
the vertebra, and from the analogy of other allied genera, it may be
inferred that they were simply articulated with the vertebre.

The pelvic arch consists, on either side, of a bone 31 inches
long, of two triangles united at their apices; the superior, 2 inches
long, is z inch broad at its upper end; the inferior, 1 inch long,
measures 12 inch along its free or lower margin, to which was arti-
culated a row of (probably five) tarsal bones, three of which remain
in position. They decrease in size towards one side, the longest of
the three being 14 inch, the shortest ¢ of an inch in length; they
are compressed at both ends, constricted and cylindrical in the
middle. To the distal smaller ends of these were articulated other
similar metatarsal bones, whose number cannot be guessed at; the
only two members of this row seen in place measure ~ of an inch
in length. To these were attached the fin-rays, long cylindrical
rods of a compact dark enamelloid substance, like that which in-
vested the vertebree and pelvic bones, and traversed by a narrow
canal. Their proximal ends are compressed; distally they taper ;
but no transverse divisions are present in any of them.

Locality: Palace, Craig. Airdrie.

to the posterior. = (in tenths).

SrrEpsopus, Huxley. Fig. 3.
~ The tooth so named has already been figured in the Journal of the

1866.] YOUNG—CARBONIFEROUS GLYPTODIPTERINES. 603 -

Tyneside Naturalists’ Club as Holoptychius sauroides, a species founded
by Agassiz, but not described by him. Its reference to Megalichthys
is equally inaccurate. The discovery of the vertebra and scales be-
longing to the tooth confirms the propriety of its erection as a
Separate genus.

The teeth vary in size, the exserted portion being ;}, to 13 inch
in height; but the smallest exhibit the characteristic form. The
ovoid laterally compressed base gradually contracts into a circular
shaft very slightly recurved, and near the apex twice bent almost at
right angles, so as to have a bayonet form; the tip is sharply
conical. ‘The convexity of the shaft and the posterior half of the
lateral surfaces are longitudinally striate; the anterior half of the
circumference is smooth. Hence it follows that the most anterior
strie are the shortest, those nearest the posterior mesial line the
longest. A narrow smooth band, equal in breadth to the interval
of any two striz, runs up the concavity; and from this the strize
depart on either side at a very small angle, tending upwards and
forwards towards the anterior surface. Their number is increased
by bifurcation, or by the intercalation of new striz ; none pass on
to the first knee-bend of the tooth. The lateral compression may be
simple or proceed to form a shallow depression which does not oc-
cupy more of the lateral surface than one-half in breadth or height,
and near the base gives the transverse section a dumb-bell shape.
The basal plications are rather rounded undulations than the sharp
folds of other Rhizodonts ; they do not interfere with the striations.

No skull has been found; but a fragment of a mandible is pre-
served, whose vertical measurement, if complete, is small in propor-
tion to the height of the tooth. Close to the alveolar margin a patch
of the outer surface remains, and shows smooth tubercles connected
by low ridges in a reticulated pattern, like that of the jaw of Rhizodus.
The mode of arrangement of the teeth is very uncertain. There
can be no doubt, however, that different sizes occurred in the same jaw,
_ the larger projecting at intervals above the smaller, as in Rhizodus.

A slab from the Fifeshire coal-field, lent me by Mr. John Young
of Glasgow, exhibits these teeth along with scales which are thin-
ner than, but essentially similar to, those of Dendroptychius. They
are cycloidal, the anterior margin is flattened, and the posterior some-
what pointed. The exposed area is relatively smaller than in Den-
droptychius, less even than in Holoptychius. The radiating grooves are
narrower, straighter, and fewer in number than in the last-described
genus, and very rarely, if ever, bifurcate. The concentric strie of
the overlapped area are faintly and equally radiated at all points.
The growth-lines are indistinct on the smooth under surface; a lon-
gitudinally oval flattened boss projects from the centre; and from
it a line frequently runs to the middle of the anterior margin,
against which the concentric lines on either side appear as if
faulted. The scales, in consequence of their delicacy, are not well
preserved: this description may afterwards, therefore, require cor-
rection ; but the main features are unmistakeable in their similarity
to those of Dendroptychius.

604 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

The vertebral characters are well marked. The vertebre are thin
osseous rings slightly constricted in the middle; the concavity of
both surfaces is shallow, and involves nearly the whole breadth.
The diameters are unequal, their difference ranging from one-fifth
to one-eighth of the longest measurement.

The notochordal foramen is also not a complete circle ; its lem
and shortest diameters coincide with those of the vertebra, of whose
area it occupies from one-fourth to a half.

The extreme examples measured in tenths of an inch are as fol-
lows :—

9 { 3
Breadth of ring ss s Breadth of foramen see
21 ' 6

In the oes the length (or antero-posterior measurement) is
between two-tenths and three- tenths at all points; but the deeper
examples show an inequality in this respect—the length at opposite
points of the ring varying considerably, as 2:5 to 2: 25 in one case,
as 4-75 to 3 inches in another.

Straight bones, similar to the neural spines of Dendroptychius,
occur in the same slab; they measure 2,1, inches in length. Asso-
ciated with scales showing the above-mentioned characters, there is
in the Andersonian Museum, Glasgow, a pectoral arch with which
are connected several bones giving attachment to long undivided
fin-rays.

Locality: English and Scottish fields, from the Coal-measures to
the Lower Limestones.

Ruomportycuivs, Huxley. Figs. 1, 2.

These scales vary from cordate-ovate to rhombic: the length in
the former case exceeds the breadth ; in the latter the reverse holds. -
In general symmetrical, the elongated scales sometimes show undue
prominence of one anterior angle. The free and overlapped surfaces -
are nearly equal in the rhombic scales; but in the cycloidal the
former is much the smaller. In both forms the punctate free sur-
face is ornamented with coarse straight ridges which follow the out-
line of the sides, meeting at an angle posteriorly, and thus giving a
rhombic aspect to the scale. The intervals of these ridges are crossed,
chiefly near the margin, by finer radial ones. The pattern may lose
its regularity—only two or three marginal ridges being complete, and
the remaining surface set with irregular tubercles. This occurs in
those scales which most nearly resemble the rhombic scales of Mega-
lichthys ; but the resemblance stops here ; for though in some speci-
mens of Megalichthys the bony surface exposed by the absence or
non-development of the enamel shows irregular tuberculation, or
even a faintly rhombic pattern like that just described, the scales
presenting these characters have their anterior area bounded by
straight lines, and do not show the cycloid outline of those of Rhom-
boptychius, those straight lines, however, which bound anteriorly
the free area being common to both. The under surface is smooth ;

s

1866. | YOUNG—CARBONIFEROUS GLYPTODIPTERINES. 605

growth lines are confined to the margin; the oval boss is sub-
central. The outer surface of these scales is finely punctate, dense,
and semilustrous.

The Andersonian Museum of Glasgow contains a large slab on
which are displayed the vertebral column and upper surface of the
cranium of this genus. About fifty vertebree are seen, of which the
anterior are the shortest and broadest, the caudal being longer
-and narrower. ‘The cranium is flattened superiorly ; its surface is
tuberculated and traversed by mucous grooves, and lines which
seem to be the sutures of the coalesced bones.

The cranial and facial portions occur as separate masses, the com-
ponents of each being intimately united. The facial portion, con-
sisting of the bones anterior to'the frontals (those, namely, which
compose the muzzle), very closely resembles that of Megalichthys and
Diplopterus. Its crescentic anterior, or intermaxillary and vomerine,
_ portion bears within and close to either outer extremity a large tooth ;
and on either side of the middle line is a similarly socketted tooth.
The small marginal teeth are continuous with two curved rows of
equally small teeth which pass in front of the outer pair of tusks,
and curving to their inner side meet in the middle line at the ante-
rior part of the basilar bar, whose surface is closely set with fine
denticles.

The cranial shield is solid; its elements, intimately united by
suture, correspond in number with those found in the cranial roof
of Megalichthys (Poiss. Foss. pl. 63). But the well-ossified ba-
silar region includes a massive basioccipital which projects be-
hind the vertical posterior wall of the cranium, and sometimes has
its length increased by the coalescence with it of at least the first
vertebral ring, whose neural processes remained distinct. The an-
terior part of the cranial is sometimes deficient, the sphenoidal (and
prootic ?) portion becoming detached. In a lateral view, the ascend-
ing alisphenoidal (?) plates and an incomplete interorbital osseous
septum are well seen.

The lower boundary of the elongated orbital space is nowhere
preserved, the only surviving parts of the lateral surface of the head
being the large opercular plates and the maxille.

The maxilla is slender in front, and sends off near its truncated
extremity a strong process directed inwards and forwards, for
articulation, probably, with the prefrontal or ethmoidal region. It
gradually expands posteriorly, and bears on the greater part of its
inferior margin, which is rounded and slightly deflected at the lower
posterior angle, a row of strong, sharp, abruptly conical teeth of uni-
form size; their bases are strongly plicate, their upper portion
usually finely reticulated. Between the maxille and the basilar
bar the roof of the mouth seems to have been closed in by a pair of
plates like those of Megalichthys, whose surface is set with fine
rasp-like teeth, bounded by a row of small, stout, conical teeth.
The connexions of these parts are nowhere seen.

The mandible is a strong bone, deep in front, tapering poste-
riorly on both margins; the transversely elongated, saddle-

606 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

shaped articular surface looks obliquely upwards and backwards,
giving, when the great length of the bone is considered (for it
reaches to nearly opposite the hinder cranial margin), an enormous
gape. The symphysial extremity is imperfect; but the arrangement
of the teeth is probably similar to that in the other genera of the
Crossopterygide; that is to say, a row of small conical teeth borders
the outer dentary margin. About the middle of the bone several
large distant teeth occur, having their sockets internal to the mar-
ginal row. These teeth are strong straight cones, plicate at the
base, surrounded at or above the middle by one or more rings of
short longitudinal furrows or pits. The inner or splenial margin
bears numerous rasp-like teeth. The splenial and dentary margins
are thus separated by an interval, considerable in front (where the
large teeth are socketed), but narrowing behind, and ceasing a little in
front of the articular end of the mandible. The outer surface of the
bone is covered with fine tubercles and less prominent connect-
ing ridges. The aspect is thus rather granular than reticulate.

The vertebra of Rhomboptychius are osseous rings, two of which
measured respectively +{ and +3 of an inch in diameter, {4 and +4
in length. The area of the notochordal foramen is three-fourths of
the whole surface, greater, therefore, than in Strepsodus, but less
than in the typical annular vertebree of Megalichthys and Rhizodopsis.
The spines associated with them on specimens in the British Mu-
seum consist of a cylindrical recurved shaft, an articular head with
convex inferior margin, and a compressed distal extremity*.

Portions of jaws are found in the same beds with the remains just
described, whose outer surface is similarly ornamented, and whose
teeth are disposed in the same way. But these teeth are remarkable
for the great breadth of their bases as compared with the rapidity
with which they taper to a fine point, often incurved.

Mrcaticutuys, Agassiz.

For the cranial and vertebral characters of this genus, and the
advance which the latter show upon the Saurodipterines with which
it is associated, I would refer to p. 12 of Prof. Huxley’s Essay,
already quoted.

The resemblance between Megalichthys and Rhomboptychius is very
close, both in cranial structure and in the arrangement of the denti-
gerous bones. Mention has been made above of palatal tooth-bearing
plates. These-are two in number, triangular, with rounded ante-
rior apex; their posterior extremity is not seen, two inches being
the greatest length to which they are exposed. Each plate bears

* In this and other genera it must be remembered that only those vertebrze
are spoken of which occur in actual association with characteristic portions of
the fishes to which they are ascribed. This caution is necessary, and, at the same
time, perhaps not always protective against error. For, on the one hand, there
are good grounds for suspecting in some genera a difference in dimensions and
even proportions of the vertebrz in the same column, and, on the other, the
presence of vertebree belonging to more than one individual is possible on the
same block. The number of vertebre still unaccounted for is large ; but it would
be both premature and out of place to enter on their description here.

1866. | YOUNG—CARBONIFEROUS GLYPTODIPTERINES. 607

a marginal row of short, very stout* conical teeth with fluted bases ;
the rest of their surface is set with similar but smaller teeth, which
are more distant over the anterior portion, but posteriorly pass into
a dense rasp of minute denticles. The connexions of these plates
are not seen; but they probably fitted into the angles formed on
either side by the maxilla and sphenoid. Since 1861, specimens illus-
trating the form of the fins have been acquired by the Museum ; but
the description and illustration of these parts are reserved, the pur-
pose of this paper being merely to give the diagnostic characters fur-
nished by the scales and teeth.

The teeth are conical, more or less incurved, and of very elegant
proportions. Both jaws, the premaxillary region above, and the an-
terior part of the mandible, contain teeth larger than the numerous
small ones which occupy the edge of the bones, and, as in Rhombo-
ptychius, form an angulated row across the roof of the mouth. The
surface of the majority is smooth; many, however, are covered with
very fine ridges, which involve ‘merely the outer portion of the
enamel, and, as Mr. Davis has pointed out to me, disappear by at-
trition. These lines are either parallel or anastomose to form a fine
reticulation; but nothing approaching the pattern of Strepsodus,
either in position or symmetry, is found. In a note read before the
Society in February, I proposed the abolition of Centrodus, M‘Coy,
on the ground that that tooth is avowedly a fragment, that it is unac-
companied by either bone or scale, and that it is identical in character
with teeth unmistakeably associated with Megalichthyic remains.
I have since had the satisfaction of finding that Mr. Davis had
arrived at the same opinion, a tablet of teeth from Carluke bearing,
as synonyms, Megalichthys and Centrodus.

The scales and head-bones of Megalichthys are covered by a layer
of smooth, porous ganoin. When this is detached by accident, the
subjacent surface of bone is also smooth, but perforated by the
larger and smaller tubes passing up from the interspaces in the
osseous substance of the scale. Such is the typical appearance ;
but in a large number of examples (fig. 6) the ganoin both of scales
and bones is patchy and incomplete, covering nearly the whole of the
surface, and only interrupted by circular spaces, which are distin-
guished by their concentrically sloping margins from the mucus-
pores, which are surrounded by a thin raised ring; or the ganoin
only occurs as scattered points. A carefully prepared section of a
scale through such an isolated patch shows that, beneath the ga-
noin, the structure is the same as in the typical Megalichthys-
scale, of which Williamson has given an excellent description. The
ganoin ceases on either side with an abruptly rounded margin, which
dips down to and stops at the average surface of the scale; for it coats
a low eminence made up of the kosmin or non-corpusculated bone,
the tufts, capillary tubes, and the upper series of Haversian canals.
Adjoining the patch the surface of the scale is smooth, and has, as in
Rhomboptychius, a close and semilustrous aspect. Under the micro-
scope it is seen that a thin layer of kosmin coats this part of the scale,
whose irregularities are formed of the upturned lamine of bone.

608 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 20,

The Haversian system is in direct communication with the surface,
giving rise to the wide pores. Sections of Rhomboptychius show the
same structure, as do those of Rhizodopsis (H. sauroides) in Wil-
liamson’s memoir. The absence of ganoin is therefore not the re-
sult of accident, but is due to the same cause in Megalichthys as in
the other two genera named—non-development.

Though the main facts regarding these genera are sufficiently well
ascertained, much still remains to be done in the working out of
their details. The statements I have made will, in all probability,
require modification and correction as better-preserved specimens
turn up.

From comparison of a large suite of specimens it appears that, while
the typical scales of Megalichthys and Rhomboptychius are sufficiently
distinct, the examples are very many which may, in the absence of
other proof, be referred to either genus. Great differences of the
scales of the same individual might account for the apparent confu-
sion ; but no specimens have been found sufficiently complete to make
this certain.

13. Note on supeoseD Burrows of Worms 7m the Laurentian Rocks
of Canapa. By J. W. Dawson, LL.D., F.R.S., F.G.S., Principal
of M‘Gill University, Montreal.

Amone other indications of fossils in the Laurentian rocks, men-
tioned in my paper on the structure of Hozoon*, are certain per-
forations. resembling burrows of worms, found in a calcareous
quartzite or impure limestone from Madoc, in Upper Canada. They
occur in specimens in the Museum of the Geological Survey, and
also in specimens subsequently collected by myself at the same
lace.

ts The beds at Madoc, containing these impressions, underlie, un-
conformably, the Lower Silurian limestones, and are regarded by
Sir W. E. Logan as belonging to a somewhat higher horizon in the
Laurentian than the Eozoon Serpentines of Grenville. They are also
less highly metamorphosed than the Laurentian rocks generally.
They are described in Sir W. E. Logan’s Report on the Geology of
Canada, 1863, at p. 32.

The impressions referred to consist of perforations approaching to
a cylindrical form, and filled with rounded siliceous sand, more or
less stained with carbonaceous and ferruginous matter, more espe-
cially near the circumference of the cylinders. These superficial
portions being harder than the containing rock, and of darker colour,
and also harder than the interior of the cylinders, project as black
rings from the weathered surfaces; but in their continuation into
the interior of the mass, they appear only as spots or lines of a
slightly darker colour, or stained with iron-rust.

When sliced transversely and examined under the microscope,
they appear as round, oval, or semicircular holes drilled through the

* Quart. Journ. Geol. Soc, Feb. 1866.

1866. | DAWSON—LAURENTIAN ANNELIDS. 609

rock, and lined around their circumference with dense and dark-
Golowred siliceous matter, while the axis, which is often of a bilobate
form, is comparatively transparent and of softer texture. The per-
forations are often at right angles to the bedding, but in some cases
nearly parallel with it.

In regard to the origin of these perforations, I suppose that they
may have been either (1) burrows of worms filled with sand sub-
sequently hardened and stained at the surface, or (2) tubes com-
posed of sand, like those of Sabella, or (3) cavities left by the
decay of Alga, and filled with sand. The first I think the most
probable view.

Figs. 1-5.—Illustrating supposed Annelid-tubes from the
Laurentian Rocks of Canada.

Fig. 1. Transverse section of Worm-burrow. Magnified, asa transparent object.

a. Caleareo-siliceous rock. | c. Sand agglutinated and stained black.
6. Space filled with calcareous spar. | d. Sand less agglutinated and unco-
loured.

Fig. 2. Transverse section of Worm-burrow on weathered surface. Natural size.
3. The same, magnified.
4. Spicule, magnified.
5. Lenticular body, magnified.

I may add that the beds at Madoc containing these supposed
fossils, hold also on their weathered surfaces impressions with rude
casts of concentric lamine, like those of Stromatopora or Hozoon,
but too obscure for determination. The limestones interstratified
with these beds also contain fragments of Hozoon, not fossilized by
serpentine, but simply by carbonate of lime, carbonaceous fibres,
spicules like those of sponges, and lenticular bodies of unknown
nature.

610

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From April 1st to June 30th, 1866.

s

I. TRANSACTIONS AND JOURNALS.

Presented by the respective Societies and Editors.

Aéronautical Society of Great Britain. 1866. Prospectus, &e.

American Geographical and Statistical Society. November 1864 to
March 1865.

American Journal of Mining. Vol.i. Nos. 2, 4-7 & 9. April to
May 1866.

Quartz and Mining, 24.

F. E. Engelhardt.—Petroleum, 25, 57.
Remarkable Volcanic Phenomena, 30.
Coal-statistics, 55.

Nova Scotia Gold, 105.

F, E. Engelhardt.—Salt, 137.

American Journal of Science. Second Series. Vol. xli. No. 122.
March 1866.

R. Pumpelly.—Geological Observations in China, Japan, and Mon-
golia, 145, ,

B. F. Mudge.—Discovery of Fossil Footmarks in the Liassic (?) For-
mation in Kansas, 174.

A. Winchell.—Geology of Petroleum in Canada West, 176.

S. W. Tyler.—Analyses of Rahtite, Marcylite, and Moronolite, 209.

C. U. Shepard.—On Scheeletine at the Southampton Lead-mine,
Massachusetts; and Uwarowite at Wood’s Chrome-mine, Texas,
215.

Geology of California, 231, 252.

G. J. Brush.—Mineralogical Notices, 246.

E. J. Chapman.—Native Lead from the North-west shore of Lake
Superior, 254.

J. S. Bliss.—Notes on Wisconsin Drift, 255.

J. D. Whitney.—Borax in California, 255.

DONATIONS. 611

American Journal of Science. Second Series. Vol. xli. No. 122
(continued).

Gigantic Marsupials of Victoria, Australia, 258.
Miscellaneous Bibliography, 284.

Assurance Magazine. Vol. xii. Part 1. April 1866.

Atheneum Journal. Nos. 2006-2018. April to June 1866.

Notices of Meetings of Scientific Societies, &c.

D. Page’s ‘Geology for General ‘Readers,’ noticed, 460.

J. Nicol’s ‘Geology and Scenery of the North of Scotland,’ noticed,
460.

G. Greenwood.—Theory of Geological Phenomena, 471.

Paleontographical Society, 471.

C. Engelhardt’s ‘Denmark in the Early Iron Age,’ noticed, 830.

B. von Cotta’s ‘Rocks Classified and Described,’ noticed, 837.

Berlin. Monatsberichte der koniglichen Preussischen Akademie der
Wissenschaften zu Berlin. 1865.

Beyrich.—Ueber einige Cephalopoden aus dem Muschelkalk der
Alpen und tiber verwandte Arten, 640.

Peters.—Ueber einen im fossilen Copalharz eingeschlossenen Gekko,
Hemidactylus, aus Zanzibar, 695.

Rose.—Ueber die Gabbro-Formation von Neurode in Schlesien, 51.

——. Ueber die Krystallform des Albits von der Roche tournée
und von Bonhomme in Savoyen in’s Besondere und des Albits im
Allgemeinen, 284.

. Monatsbericht der kéniglichen Preussischen Akademie der
Wissenschaften. January 1866.
Beyrich.—Ueber ein neues Skelet des Pterodactylus longirostris, 16.

——. Sitzungsberichte der Gesellschaft naturforschender Freunde.
1860-62 and 1865.

——. Zeitschrift fiir die gesammten Naturwissenschaften. Vol.
xxiv. 1864.
W. E. v. Braun.—Beitrage zur Kenntniss der sphiroidischen Con-
cretionen des kohlensauren Kalkes, 97.
Siewert.—Ueber die Trennung von Cadmium, 399.

Vol. xxv. 1865.

F. Bode.—Die Steinkohlenformation bei Plotz, 233 (plate).

W. Heintz.—Bemerkungen tber den Stassfurtit, 404.

A. Steinbeck.—Ueber den Stassfurtit, 397.

G. Suckow.—Notizen zu Erganzungsfarbenphanomenon und mine-
ralischen Metamorphosen, 143.

Vol. xxvi. 1865.

G. Suckow.—Ueber die Aufgabe der Mineralogie, 239.

Bremen. Erster Jahresbericht des naturwissenschaftlichen Vereines.
1866.

Calcutta. Journal of the Asiatic Society of Bengal, Part I. No. 4,
and Part II. No. 4. 1865.

—
e

612 DONATIONS.

Canadian Journal. New Series. Vol. xi. No. 62. April 1866.

Chemical Society. Journal. Second Series. Vol. iv. Nos. 39-42.
March to June 1866.

A. H. Church.—Chemical Researches on New and Rare Cornish
Minerals, 1380. |
J. A. Wanklyn and E. T. Chapman.—Magnesium, 141.

Colliery Guardian. Vol. xi. Nos. 275-287. April to June 1866.

Notices of Meetings of Geological Societies.

Oil-wells in Russia, 254.

Geological History of the Surface of Land, 255.

Origin of Coal, 255.

Coal-supply of Europe and America, 259, 276.

i. H. Birkenhead.—Geology of the Lancashire Coal-fields, 261.

Maryland Coal-fields, 258.

Leinster Coal-field, 315.

Anthracite in California, 363.

American Coal-statistics, 385.

Discovery of Coal on the shores of the Red Sea, 407.

J. Randall.—Petroleum in Shropshire, 408.

Ironstone in the Wigan four-feet coal, 408.

Origin of Petroleum, 463, 466.

J. Holdsworth’s ‘ Extension of the English Coal-fields beneath the
Secondary Formations of the Midland Counties, &c.,’ noticed, 465.

Cornwall. Royal Geological Society. 48th, 49th, and 50th Annual
Reports and Transactions. 1865.
W. Pengelly.—Geological Age of the Dartmoor Granites, 419.
HK. Carne.—Geology of Mentone, 433.
W. Pengelly.—Co-relation of the Slates and Limestones of Devon
and Cornwall with the Old Red Sandstone of Scotland, 441.
. Supposed Uniform Height of Contemporary Raised Beaches,
446,
S. Higes, jun.—Notice of a Chalk Flint (?) found in the Balles-
widden Mine, St. Just, 448.

Darmstadt. Notizblatt des Vereins fir Erdkunde. Vol. ii. Heft 4.
1865,

R. Ludwig.—Untersuchung von Versteinerungen des Mainzer
Beckens, 47.
Versteinerungen im Stringocephalenkalke bei Waldgirmes,

62.
Die Fischreste im tertidiren Meeresthone bei Nierstein, 80.
Langsdorf.—Basalt und Buntsandstein auf dem Otzberg, 80.

R. Ludwig.—Melaphyr in der Nahe von Frankfurt, 95.
Langsdorf.—Basalt und Buntsandstein bei Eisenbach, 95.
Rh. Ludwig.—Stringocephalenkalk und Cramenzelschiefer der Devo-
nischen Formation zwischen Langgéns, Butzbach und Holzheim,
95.
——. Der Septarienthon (Beyrich) tiber den Braunkohlen mit

Glyptostrobus Huropeus bei Zell im Vogelsberge, 157.

—. Melaphyrgang im Granit an der Stiftsstrasse in Darmstadt,

Fuchs.—Die vulecanischen Erscheinungen der Erde, 191.
Zincken.—Die Braunkohle und ihre Verwendung, 192.

DONATIONS. 613

Dublin. Royal Society. Journal. Vol. iv. No. 34. 1865.

Geological Magazine. Vol. ii. Nos.4 &6, April and June 1866.

F. W. Hutton.—Geology of the Island of Malta, 145 (2 plates).

T. R. Jones.—Specimens from Malta, 151.

P. B. Brodie.—Deposit of Phosphatic Nodules in Bedfordshire, 1538,

D. Mackintosh._Sea against Rivers, or the Origin of Valleys, 155.

H. Wyatt-Edgell—_New Species of Lichas, &c., from the Llandeilo
Flags, 160.

Ae ee Church —N otes on Chinese Figure-stones, 164.

D. Page’s ‘Geology for General Readers,’ noticed, 175.

J. Nicol’s ‘Geology and Scenery of Scotland,’ noticed, 177.

G. P. Scrope.—Origin of Hills and Valleys, 241.

A. Geikie.—Permian Volcanos in Scotland, 243.

W. Carruthers.—Fossil Araucarian Cones, 249 (plate).

G. Maw.—Tufa-deposits in Flintshire, 253.

Monographs of the Patzeontographical Society, 259.

Quarterly Journal of the Geological Society, 261.

Notices of Memoirs, 165, 256.

Reports and Proceedings, 178, 268.

Correspondence, 184, 275.

Miscellaneous, 189, 284.

Obituary Notices, 192, 288,

Geological and Natural History Repertory. Vol.i. Nos. 12-14.
April to June 1866.
Proceedings of Societies, 244.
T. Baines.—Flint-flakes in the Drift and manufacture of Stone

Implements by the Australians, 258.
Notes and Queries, 264.

Geological and Polytechnic Society of the West Riding of Yorkshire.
Report of Proceedings. 1864-65.

HE. Tindall.—On an Ancient Barrow or Tumulus, and Flint Imple-
ments, found near Bridlington, 387.

P. Cooper.—Kffects of certain Geological Arrangements on the
working of Coal, 394.

J. Farrer.—Further Explorations in the Dowkerbottom Caves, in
Craven, 414.

_ Geologists’ Association. Proceedings. Part 1. 1866,

C. T. Richardson.—Past, Present, and Future of Geology, 1.

C. C. Blake.—Geological Evidences of the Present Domesticated
Animals, 6,

A. Bott.—Lepidotus Fitton, 12.

J. Rofe.—The Starr Hills of the Lancashire Coast, 18.

R. J. L. Guppy.—Certain River-bars and Lagoons on the Coast of
New Zealand, 16.

Heidelberg. Verhandlungen des naturhistorisch-medizinischen Ver-
ems. Yol.iy. Part 2. 1866.
Fuchs.—Ueber die Natur der Lava, 25.
Institution of Civil Engineers. Abstracts of Proceedings, Session
1865-66. Nos. 15 & 16.
G. R. Burnell. Water-supply of Paris.

614 DONATIONS,

Intellectual Observer. Vol. ix. Nos. 51-53. April to June 1866.

Mastodon and Elephant, 239.

W oodwardite, 240.

Discovery of an Entire Mammoth, 240.

D. T. Ansted.— Winter Visit to Mount Etna, 268.

Leeds Philosophical and Literary Society. Annual Report for 1864—
65.

Catalogue of the Library.

Linnean Society. Journal. Vol. ix. No. 33 (Zoology) and No. 37
(Botany). 1866.

Liverpool Literary and Philosophical Society. Proceedings. No. 19.
1864-65.
W. Ferguson.—Geological Notes on the Aberdeenshire Coast, 162.

London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xxxi. Nos. 209-212. April to June (with Sup-
plementary Number) 1866.

J. Croll_—Physical Cause of the Submergence and Emergence of the
Land during the Glacial Epoch, 501.

Geological Society. Abstracts of Proceedings, 318, 477, 545.

J. C. Moore —Glacial Submergence, 372.

S. Haughton.—Change of Eccentricity of the Earth’s Orbit regarded
as a Cause of Change of Climate, 374.

Pratt.—The Fluid Theory of the Earth, 430.

The Level of the Sea during the Glacial Epoch, 532.

London Review. Vol. xii. Nos. 301-318. April to June 1866.
Notices of Meetings of Scientific Societies, &c.
Mines of Cornwall and Devon, 402.
Manchester Geological Society. Transactions. Vol. v. No. 13.
1865-66.
G. C. Greenwell.—On some Coal plants, 194.
C. Hardwick.—Geology in its relation to Archeology, 201.
J. Plant and E. Williamson. —Geology and Fossils of the Lingula-
flags, or Primordial Zone, of the Gold-districts of North Wales,
220 (plate).

Microscopical Society. Address of the President, James Glaisher,
Esq., F.R.S. 1866.

——, Jast of Members. 1865.

Munich. Sitzungsberichte der kénigl.-bayer. Akademie der Wissen-
schaften. 1865. Vol.u. Hefte 3 & 4.

V. Kobell.—Ueber den Klipstenit, ein neues Mangansilicat, 340.
C. W. Giimbel.—Ueber das Vorkommen von unteren Triasschichten
in Hochasien, 348 (plate).

1866. Vol. i. Hefte 1 & 2.
C. W. Giimbel.—Das Vorkommen von Eozodn in dem ostbhayerischen
Urgebirge, 25 (3 plates).

DONATIONS. 615

Northumberland and Durham. Natural History Transactions of.
wom Part lt. 1365.

J. W. Kirkby.—Remains of Fish and Plants from the “ Upper Lime-
stone” of the Permian Series of Durham, 64 (plate).

Paleontographical Society. Monographs of British Fossils. Vol.
xvi. For the year 1864. 1866.

A Monograph of the British Fossil Echinodermata from the Oolitic
Formations. Vol. ii. Part 2. On the Ophiuroidea. By Thomas
Wright.

A Monoeraph of British Trilobites. Part 3. By J. W. Salter.

A Monograph of British Belemnitide. Part 2. By John Phillips.

The British Pleistocene Mammalia. Part 1. By W. Boyd Dawkins
and W. Ayshford Sanford.

Paris. Annales des Mines. 6°Série. Vol. viii. Livr.5 & 6. 1865.

Daubrée.—Extraits de minéralogie, 219.
Delesse et de Lapparent.—Extraits de Géologie, 307, 597.

Vol. ix: ivr. 1” 1866:

Bulletin de la Société Géologique de France. 2° Série.
Vol. xxiii. Feuilles 1-5. 1866.

D’Omalius d’Halloy.—Sur une découverte, & Mons, d’un calcaire
grossier avec fossiles semblables & ceux du calcaire grossier de
Paris, 12.

Toucas.—Sur 1’infra-lias du Beausset (Var), 18.

Virlet.—Sur la topographie et la géologie du Mexique et de l’Amé-
rique centrale, 14.

L. Pillet.—Le terrain argovien aus environs de Chambéry, 50.

Arnaud.—Des argiles lignitiféres du Sarladais, 59.

Levallois.—Sur la découverte, par MM. A. Falsan et A. Locard, de
deux lits 4 ossements dans le Mont-d’Or Lyonnais, 64.

Edm. Pellat.—Sur la communication précédente, 66.

A. Boué.—Sur les environs de Lahr, 70 (plate).

J. J. Bianconi.—Sur l’ancien exhaussement du bassin de la Méditer-
ranée, 72,

A. Locard.—Sur la présence de deux bone-beds dans le Mont-d’Or.
Lyonnais, 80.

Philadelphia. Academy of Natural Sciences. Proceedings, 1865.
Nos. 1-5. January to December.

F. B. Meek and A. H. Worthen.—New Types of Organic remains
from the Coal-measures of Illinois, 41.

T. A. Conrad.—Eocene Lignite Formation of the United States, 70.

Catalogue of the Hocene Annulata, Foraminifera, Echinoder-
mata, and Cirripedia of the United States, 73.

A. Winchell.—New species of Fossils from the Marshall Group of
Michigan, and its supposed equivalents in other States, 109.

EK. D. Cope.—Amphibamus grandiceps, a new Batrachian from the
Coal-measures, 134.

¥. aaa and A. H. Worthen.—Remarks on the Genus Taxocrmus,

Descriptions of new species of Crinoidea, &c., from the
Paleozoic Rocks of Illinois, 148, 155. .
F. B. Meek.—On the genus Gilbertsocrinus, 166.
VOL. XXII,——PART I,

h
ka

616 DONATIONS,

Philadelphia. Academy of Natural Sciences. Proceedings, 1865.
Nos. 1-5 (continued). .
T, A. Conrad.—Observations on American Fossils, with Descriptions
of two new species, 184.
F, B. Meek and A. H. Worthen.—Paleontology of Illinois and other
Western States, 245,
F’. B. Meek.—Microscopic Shell-structure of Spirifer cuspidatus, Sow.,
&e., 275,
Photographic Journal. Vol. xi. Nos. 168-170. April to June
1866.

Puy. Annales de la Société d’Agriculture, Sciences, Arts et Com-
merce. “Vol, xxv, 1862)

NOL xexvae OO:

Quarterly Journal of Microscopical Science. New Series. Yol. xiv.
No. 22. April 1866.

Quarterly Journal of Science. Vol. ii. No. 10. April 1866.
Darwin and his Teachings, 151 (lithographic portrait).
C. Daubeny.—Antiquity of the Volcanos of Auvergne, 199.
Reader. Vol. vii. Nos. 171-184. April to June 1866.

Notices of Meetings of Scientific Societies, &c. ;

D. T. Ansted’s ‘Physical Geography and Geology of Leicestershire,’
noticed, 351.

Physical Aspect of Palestine, 376.

R. I. Murchison.—Geology of the North of Scotland, 377.

Theory of Geological Phenomena, 499.

W. B. Dawkins and W. A. Sanford’s ‘ British Pleistocene Mammalia,’
noticed, 422.

C. M. Doughty.—Glaciers of Norway, 566.

Royal Asiatic Society of Great Britain and Ireland. New Series.
Volo. Part 1s 1366,

Royal Geographical Society. Proceedings. Vol. x. No.3. May
1866.
Schmidt.—Volcanic Eruptions in Santorin, 118.
——. Journal, Vol. xxxy. 1865.
J. F. Wilson. Water-supply of the Orange River Basin, 106 (map).
Royal Horticultural Society. Journal. New Series, Vol.i. Part 2.
April 1866.
_——. Proceedings. New Series. Vol. i. Nos. 3-6. March to
June 1866.

Royal Institution. Proceedings. Vol. iv. Part 3. 1866.
W. Pengelly.—Kent’s Cavern, Torquay, 534.

Royal Society. Proceedings. Vol. xv. Nos. 82-84. 1866.
J. Evans.—Possible Geological Cause of Changes in the Position of
the Axis of the Earth’s Crust, 46.
C. E. von Baer.—Discovery of the Body of a Mammoth in Arctic
Siberia, 93.
W. B. Dawkins.—Dentition of Rhinoceros leptorhinus, Owen, 106.
C. Schorlemmer,—Amyl-compounds from Petroleum, 131,

DONATIONS. 617

Royal Society. ‘Transactions. Vol. cliv. 1864-65.

J. Prestwich.—Theoretical Considerations on the Conditions under
which the (Drift) Deposits containing the Remains of Extinct
Mammalia and Flint Implements were accumulated, and on their
Geological Age, 247 (2 plates). :

S. Haughton.—Joint-systems of Ireland and Cornwall, and their
Mechanical Origin, 393.

ea «| Vol, cly. Parts L & 2. 1866.

T. H. Huxley.—Osteology of the genus Gilyptodon, 31 (6 plates).

KE. W. Binney.—Description of some Fossil Plants, showing Struc-
ture, found in the Lower Coal-seams of Lancashire and Yorkshire
579 (6 plates). :

——. List of Fellows, Foreign Members, &e. 1865.

St. Petersburg. Verhandlungen der kaiserlichen Gesellschaft fiir die
gesammte Mineralogie. Jahrgang 1863. 1864.

H. Rose.—Ueber den Samarskit, 1. .

N. Barbot de Marni.—Beschreibung der Astrachan’schen oder Kal-
micken Steppe, 15 (coloured map).

C. Pander.—Geognostische Beobachtungen auf der Ssamara’schen
Biegung, 121 (coloured map). }

P. W. Jeremejew.—Beschreibung einiger Andalusite russischer Fun-
dorte, 135.

K. v. Hoffmann.—Der Jura in der Umgegend von Mezkaja Sasch-
tschita im Orenburg’schen Gouvernement, 148 (7 plates).

Scientific Opinion. Vol.i. Nos. 1-3. April to June. 1866.

Notices of Meetings of Scientific Societies, &c.

D. Mackintosh.—Geology of the Moon, 4.

D, Page’s ‘Geology for General Readers,’ noticed, 11.
Coal in London, 39.

F. W. Hutton.—Geological History of Malta, 53,

Shanghai. Journal of the North-China Branch of the Royal Asiatic
Society. New Series. No. 2. December 1865,

Lamprey.—Geology of the Great Plain, 1 (map).
T. W. Kingsmill.— Geology of a portion of Quang-Tung, 21 (map).

Society of Arts. Journal. Vol. xiv. Nos. 698-710. April to June
1866. :
Coal in China, 450; in Queensland, 479.
Origin of Petroleum, 479.
The Coal Question, 490,
Copper Trade, 491.
Liverpool Coal Trade, 494,
Eruption produced by an Artesian Well, 495.
Bismuth in New Zealand, 550.

Turin. Atti della R. Accademia delle Scienze. Vol. i, Parts 1 & 2.
1866. .
2 2

618 DONATIONS.

- Turin. Memoric della Reale Accademia delle Scienze. 2° Serie.
Vol. xxi.

Perazzii—Sul concentramento della calcopirite nel giacimento di
pirottina nichelifera di Miggiando, e sulla paragenesi dei minerali
cristallizzati che vi si trovano, 67.

E. Sismonda e De Filippi—Disquisizioni paleontologiche intorno ai
Covallarii fossili delle rocce terziarie del distretto di Messina, 73
(14 plates).

La Marmora e EH. Sismonda.—Nota intorno ai giacimenti cupriferi
contenuti nei monti serpentinosi dell’ Italia centrale, 396.

G. Seguenza.—Disquisizioni paleontologiche intorno ai Corallarii fos-
sili delle rocce terziarie del distretto di Messina, 399.

Vienna. Denkschriften der kaiserlichen Akademie der Wissenschaf-
tem. . Volt xxive > 1865.
Zittel.— Die Bivalven der Gosaugebilde in den nordéstlichen Alpen,

105 (11 plates).
Laube. Sone Fauna der Schichten von St. Cassian, 225 (10 plates).

Sitzungsberichte der kaiserlichen Akademie der Wissenschaf-
ten. Vol. li. Hefte 83-5. -Abth.1. 1865.

Unger. —Sylloge plantarum fossilium, 196.

R. von Ettingshausen.—Die fossile Flora des mihrischschlesischen
Dachschiefers, 201.

Suess.—Ueber die Cephalopoden-Sippe Acanthoteuthis, R.Wagn., 225
4 plates

oe ee Fauna der Schichten von St. Cassian. Abth. IL., 253.

Boué.—Vergleichung gewisser ehemaligen geologischen Phiinomene
mit einigen unserer Zeit, 323.

Unger. —Ueber einige fossile Pflanzenreste aus Siebenbiirgen und

Ungarn, 3713.

Reuss.—Zwei neue Anthozoen aus den Hallstadter Schichten, 381
(4 plates).

xenon Ke rystallographische Studien tiber den Antimonit, 456 (11
plates

=e «VOL I. Mette 8-5. (A bth. i. Bleoo:
Vol. Hi. Mette 1G 2) dni eee

Boué.—Ueber die mineralogisch-paliontologische Bestimmung der
geologischen Gebilde, sammt eispielen” ihrer Anwendung zur
Feststellung der Geologie des Erdballes, 31.

Suess.—Ueher Ammoniten, Paruelerie

Stoliezka.—Hine Revision der Gastropoden der Gosauschichten j in
den Ostalpen, 104 (plate).

es .—Die Bivalven der Gosaugebilde in den nordéstlichen Alpen,
226.

Zepharovich.—Kvystallographische tee aus den chemis-
chen Laboratorien zu Graz und Prag, 237.

Tschermak.—Ueber das Auftreten vou Olivin im Augitporphyr und
Melaphyr, 265.

Register zu den Banden 48 bis 50 der Sitzungsberichte der
math. tna Classe der k, Akad, der Wissenschaften, 1865.

DONATIONS. 619

Vienna. Kaiserliche Akademie der Wissenschaften in Wien. Ab-
stracts of Proceedings. Nos. 8-13. 1866.

Tschermak.—Ueber Pseudomorphosen der Mineralien, 109.
G. Laube.—Fauna der Schichten von St. Cassian, 123.

. Jahrbuch der k.-k. geologischen Reichsanstalt. Vol. xvi.
No. 1. January to March 1866.

H. Hofer.—Beitrage zur Kenntniss der Trachyte und der Hrznieder-
lage zu Nagyag in Siebenburgen, 1.

M. von Hantken.—Die Tertiarbilde der Gegend westlich von Ofen, 25.

I. vy. Hechstetter.—Zur Erinnerung an Dr. Albert Oppel, 59.

EK. F. von Sommaruga.—Chemische Zusammensetzung des Wiener
Tegels, 68. °

A. Pichler.—Cardita-Schichten und Hauptdolomit, 73.

J. Szab6.—Die Trachyte und Rhyolithe der Umgebung von Tokaj, 82.

J. Cermak.—Die Braunkohlenablagerungen von Handlova, 98.

TF’. Babanek.—Die nordlichen Theile des Trentschiner Comitates, 105.

Verhandlungen der k.-k. geologischen Reichsanstalt 1866.

Warwickshire Naturalists’ Field-club. Proceedings. 1865.

J. Parker.—Bone-caves of Liége, 1.

P. B. Brodie.-—Remarks on three outliers of Lias in North Shrop-
shire and South Cheshire, Staffordshire, and Cumberland, and
their correlation with the main range, 6.

Wiesbaden. Jahrbiicher des Vereins fir Naturkunde im Herzog-
thum Nassau. Parts 17 &18. 1862-68.

TI, PERIODICALS PURCHASED FOR THE LIBRARY.

Annales des Sciences Naturelles. Zoologie. Vol.i. 1824.

J. Desnoyers.—Nouvelles observations sur le terrain qui contient en
Normandie (département de l’Orne), le bois fossile & odeur de
truffes, 58 (plate).

L. Pareto.—Note sur les bassins tertiaires, 86.

Dangerfield.—Apercu géologique de la province de Malwa (Inde
centrale, 249,

Brongniart.—Sur le mémoire de M. Constant Prevost “Sur la
Géologie des Falaises de Normandie, 293.

Desmarest.—Note sur la nécessité de retirer le corps organisé nommé
Amphitoite, de la série des Fossiles animaux, 331.

J. de Charpentier.—H sai sur la constitution geognostique des Pyré-
nées, 451,

——. —. Vol.u. 1824,

A. Boué.—Sur les dépots Tertiaires et Basaltiques de la partic du
Wirtemberg et de la Baviére, au nord du Danube, 5.

620

DONATIONS.

Annales des Sciences Naturelles. Zoologie. Vol. ii. (continued).

L. Dufour.—Sur l’Alumine hydratée silicifére ou Lenzinite des envi-
rons de Saint-Sever, 21.

C. P. Ollivier.—Sur un nouveau gissement du Bitume élastique, 149.

A. Boué.—Mémoire géologique sur les Terrains anciens et secondaires
du sud-ouest de Allemagne, au nord du Danube, 175.

Mémoire géologique sur le sud-ouest de la France suivi de
quelques observations comparatives sur le nord du meme royaume,
et surtout sur les bords du Rhin, 387.

Cuvier.—Sur des os de Séche fossiles, 486 (plate).

——. ye Mole, 18240).

——,

E. Mitscherlich.—Sur la méthode de calculer les angles des Cristaux
et le rapport de position de leur faces, 149 (plate).

J. J. N. Huot.—Sur le banc de Grignon, sur le Calcaire renfermant
des restes de végétaux, et sur les couches supérieures de cette
localité, 5.

Note Géologique sur le prétendu Fossile Humain trouvé prés
de Moret (Seine et Marne), 158.

A. Boué.—Mémoire Géologique sur le sud-est de la France, suivi de
quelques observations comparatives sur le nord du méme royaume,
et surtout sur les bords du Rhin, 55, 299.

A. Brongniart.—Sur un Mémoire de M. Bonnard, intitulé “ Notice
eéologique sur quelques parties de la Bourgogne,” 456 (plate).

C. Prévost.—Sur une Ichthyolithe des rochers des Vaches-Noires,
243.

V. Jacquemont.—Sur le gissement du Gypse de la cote orientale du
Groenland, 170. -

Vole iv.) SZ:

M. de Rivero.—Analyse de l’eau du Rio-Vinagre dans les andes de
Popayan, 66.

A. de Humboldt.—Sur quelques phénomeénes que présentent le soufre,
Vhydrogéne sulfuré et l’eau dans les volcans, 66.

De quelques phénomenes physiques et géologiques qu’offrent

les Cordilliéres des Andes de Quito et la partie occidentale de

VHimalaya, 225.

_ L. von Buch.—Note sur Vile de Madére, 14.

A. Boué.—Mémoire géologique sur le sud-ouest de la France et par-
ticuliérement sur une Oolite a fougéres de Mamers dans le départe-
ment de la Sarthe, 353. |

C. Prévost.—Sur les Schistes calcaires Oolitiques de Stonesfield en
Angleterre, dans lesquels ont été trouvés plusieurs ossemens fossiles
de Mammiferes, 389 (plate).

W. Webster.—Sur la constitution géologique des environs de Boston,
253.

De Basterot.—Mémoire géologique sur les environs de Bordeaux.
-]e partie comprenant les observations générales sur les mollusques
fossiles, et la description particuliére de ceux qu’on rencontre dans
ce bassin, 492.

Ad. Brongniart.—Sur les végétaux fossiles renfermés dans les Grés
de Hoer en Scanie, 200 (plate).

. Sur les végétaux fossiles de l’Oolite 4 Fougéres, de Mamers,
416 (plate).

-——. Sur les végétaux fossiles du terrain houiller, et sur leurs rap-
ports avec les végétaux vivans, 23 (plate).

DONATIONS. 621

Annales des Sciences Naturelles. Zoologie. Vol.v. 1825.

Berzelius.—Des changemens dans le systeme de Minéralogie Chi-
mique, qui doivent nécessairement résulter de la propriété que pos-
sédent les corps isomorphes, de se remplacer mutuellement en
proportions indéfinies, 235.

Bonnard.—Sur une nouvelle Chaux phosphatée terreuse, 319.

Vauquelin.—Examen d’une nouvelle variété de Wolfram ou Schéelin
ferruginé, 110. 7

Note sur analyse d’un échantillon de Phosphate de Manga-
nése et de fer, 112.

De Humboldt.—Sur le Platine de Sibérie, 111.

. Sur la présence du Sélénium dans divers Minéraux, 324.

C. P. Ollivier—Sur un Sable oxidulé Titanifére des bords de La
Loire, 329.

Marcel de Serres.—Sur des cavernes de Calcaire grossier 4 ossemens,
découvertes dans les environs de Lunel-Vieil, prés de Montpellier

Hérault), 330.

D’Orbigny.—Notice sur les becs de Céphalopodes fossiles, 211 (plate).

Sur deux espéces du genre Ptérocére, observées dans le Cal-
Caine Jurassique du département de la Charente-Inférieure, 188

late).

@, P. are les genres Hippurite et Radiolite, 205.

I’, Soret.—Catalogue raisonné des variétés d’Amphibole et de Pyro-
xéne, provenant du Wolfsberg, prés Czerlochin Bohéme, 387.

A. Crichton.—Sur le climat du monde antédiluvien, sur son indepen-
dance de l’influence solaire, et sur la formation du Granite, 391.
Alex. Brongniart.—Observations sur diverses espéces Minérales, 430.

L. P. Walmstedt.—Examen chimique du Péridot, 461.

Basoche.—Sur quelques Fossiles du terrain intermédiaire des environs
de Falaise, 473.

eee ee

Vol. vi. 1825.

G. A. Mantell.—Sur l’Iguanodon, reptile fossile nouvellement décou-
vert dans le grés de la forét de Tilgate, Sussex, 124 (plate).

Marcel de Serres.—Sur une Caverne 4 ossemens fossiles, 518.

Stromeyer et Haussman.—Analyse du Séléniure de Plomb natif,
103.

Delafosse.—Sur la méthode générale du Rév. W. Whewell pour cal-
culer les angles des cristaux, 121.

Wohler.—Sur l’analyse du plomb phosphaté et du plomb arséniaté,
et sur la présence du Chlore dans ces minéraux, 240.

Vauquelin.—Nouvelle analyse de la Dioptase, 355,

Dubuisson.—Sur les dépdts de Grés et de Poudingues, 488.

Anon.—Note sur la présence de l’Iode dans un certain nombre d’Kaux
minérales, 508.

Vauquelin.—Note sur la Découverte d’un Iodure d’argent natif, 510.

Anon.—Note sur le Carbonate de soude natif, 511.

——. —-. Vol.vi. 1826.

Dufresnoy et Elie de Beaumont.—Sur la Constitution géognostique
et les gites métalliféres du Cornouailles et du Devonshire, 195
(plate).

Bertrand-Geslin.—Note sur la Caverne d’Adelsberg, en Carniole, 458.

Laugier.—Analyse de deux Pierres magnésiennes provenant des mon-
tagnes d’Ollioules en Provence et de Cette en Languedoc, 243,

622 DONATIONS.

Annales des Sciences Naturelles. Zoologie. Vol. viii. 1826.

H. Ferrand.—Itinéraire eéognostique de Fontainebleau a Chateau-
Landon, 54 (2 plates).

Hérault.—Sur le terrain d’Alengon et de ses environs, 101.

Brard.—Sur la prétendue Mine d’étain de Ségur, 111.

Alex. Brongniart.—De l’Arkose. Caractéres minéralogiques et géo-
logiques de cette roche, 113 (plate).

De Rasoumowsky.—Sur les Trilobites et leurs Gisements, 186 (plate).

S. de Bustamente.—Mémoire sur de nouvelles variétés de Chaux car-
bonatée et d’Argent sulfuré du Mexique, 205 (plate).

Gaillardot.—Sur quelques Fossiles du grés bigarré, 286 (plate).

Alluand.—Notice sur l’Hétérosite, ?Hureaulite (fer et manganése
phosphatés), et sur quelques Minéraux du département de la
Haute-Vienne, 334,

Alex. Brongniart.—Sur la Bustamite, bisilicate de manganése et de
chaux du Mexique, 411.

J. Part.—Description du Squelette du Daim fossile d’Irlande (Cervus
megaceros), 389 (plate).

Wol. ix. 1326:

Marcel de Serres.—Sur la Présence de deux genres de Pachydermes,
Cheropotame et Paleotherium, dans les bréches de Séte (Hérault)
et de Villefranche-Lauraguais (Haute-Garonne), 191.

Bertrand-Geslin.—Sur la Caverne 4 Ossemens de Banwell, 196 (plate).

Marcel de Serres.—Note sur les Cavernes 4 Ossemens et les Bréches
osseuses du midi de la France, 200 (plate).

Anon.—Sur la présence de l’Anatase dans les mines de diamant du
Brésil, 228.

Studer.—Matériaux pour servir a une Monographie de la Molasse, ou
Recherches géognostiques sur les Roches et les Corps fossiles qu’on
trouve entre les Alpes et le Jura, 252.

Cuvier.—Ossemens fossiles du Puy-de-Dome, 273.

Dubreuil et Marcel de Serres.—Note sur un Calcaire d’eau douce,
renfermant des débris de tortues de terre, 394.

Nolex. 1327.

Marcel de Serres, Dubreuil, et De Christol—Note sur un Fémur de
MaStodone a dents étroites (Mastodon angustidens) découvert dans
les terrains marins supérieurs des environs de Montpellier, 216.

L. von Buch.—Sur quelques Phénomeénes géognostiques que présente
la position relative du porphyre et des calcaires dans les environs
du lac de Lugano, 195.

W. Buckland.—Relation @’une découverte récente d’os fossiles faite
dans la partie orientale de la France, 306 (plate).

N. Menge.—Sur les Mines d’or et de Platine des monts Ourals, 386.

i. de Beaumont.—Sur la constitution géologique des iles Baléares,
423 (plate).

Volos.” L827.

B. Studer.—Remarques géognostiques sur quelques Parties de la
chaine septentrionale des Alpes, 5.

Analyse de quelques Dolomies, 112.

A. Fargeau.—sSur la grotte d’Osselles, 236,

B. Studer.—Notice géognostique sur quelques Parties de la chaine
du Stockhorn, et sur la Houille du Simmenthal, 249 (plate); sur
les Coquilles fossiles qui se trouvent dans les terrains décrits, 266.

Alex. Brongniart.—Sur les époques géognostiques qu’elles indiquent,
et sur la montagne de Diablerets, 266,

DONATIONS, 623

Annales des Sciences Naturelles. Zoologie. Vol. xi. (continued).

Brounner.—Analyse de la Houille de Boltigen, 280.

Marcel de Serres.—Sur la série des terrains tertiaires du midi de la
France, 325.

Sur les Terrains d’eau douce découverts récemment dans les

environs de Séte, 393. |

Vol sie i827)

Tournal.—Sur deux cayernes 4 ossemens découvertes a Bize, dans les
environs de Narbonne, 78.

Teissier.—Sur un Terrain renfermant de nombreux débris de Mollus-
ques et de reptiles 4 Brignon, 197.

Alex. Brongniart.—Sur le mémoire précédent, 207.

De Bonnard.—Sur la constance des faits géognostiques qui accom-
pagnent le terrain d’arkose dans l’est de la France, 298.

———_—

See, «Vol. xi, 1828.

Marcel de Serres.—Sur un fémur de Mastodonte 4 dents étroites
(Mastodon angustidens) découvert dans les sables marins qui com-
posent l’étage le plus éléve des terrains marins supérieurs des envi-
rons de Perpignan, 73.

W. Buckland.—Note sur des traces de Tortues observées dans le grés
rouge, 85.

Dujardin.—Sur la constitution géognostique de la Touraine, 122.

J. de Christol et A. Bravard.—Sur quelques espéces nouvelles
d’Hyeénes fossiles découvertes dans la caverne de Lunel-Viel prés
Montpellier, 141.

Alex. Brongniart.—Sur la présence de la Webstérite dans l’argile
plastique d’Auteuil prés Paris, 225.

Deshayes.—Sur le Strophostome, nouveau genre de coquilles fossiles
de la famille des Hélices, 282 (plate).

Ad. Brongniart.—Sur la présence du Pecopteris reticulata dans les
mémes couches en Angleterre et en France, 335.

Dufresnoy.—Sur existence du gypse et de divers minerais métal-
liféres dans la partie supérieure du lias du Sud-Ouest de la France, .
394 (plate).

C. de Montbret.—Sur quelques montagnes du Haut-Pérou, 420,

Dufresnoy.—Sur la Glaubérite de la mine de sel de Vic, 444.

—., evV olive L628;

Alex. Broneniart.—Notice sur les blocs de rocher des terrains de
transport de Suéde, 5 (map).

J. Teissier.—Sur les terrains d’Arkose, des environs d’Anduze, dans
le département du Gard, 68.

Dufrénoy.—Sur la Couzeranite, 72.

H. Duncan.—Sur les traces de pieds d’animaux imprimés dang le
eres de la carriére de Corncokle-Muir, Dumfries, 103.

EK. de Beaumont.—Sur un gisement de végétaux fossiles et de Bélem-
nites, situé 4 Petit-Cceur, 113.

Ad. Brongniart.—Sur les végétaux fossiles des terrains d’anthracite
des Alpes, 127.

Ki. de Beaumont.—Mémoire sur les différentes formations qui, dans
le systéme des Vosges, séparent la formation houilliére du has, 258,

W. Buckland.—Sur une collection de fossiles, végétaux et animaux,
et de roches du pays des Birmans, 283,

624 DONATIONS,

Annales des Sciences Naturelles. Zoologie. Vol. xiv. (continued).
Clift.—Sur les restes fossiles de deux espéces nouvelles de Mastedonte
et d’autres animaux vertébrés, trouvés sur la rive gauche de
VIrawadi, 288.
Bertrand-Geslin.—Sur le terrain de transport 4 ossemens du Val
d’Arno Supérieur, Toseane, 365.
A. del Rio.—Notice sur deux nouveaux minéraux découverts a
Culebras, au Mexique, 371.
W. J. Broderip.—Sur le machoire d’un Mammifére trouvée dans le
schiste de Stonesfield, 374 (plate).
W. H. Fitton.—Sur les couches des carriéres de Stonesfield, qui ren-
ferment les ossemens de mammifeéres, 378.
Alex. Brongniart.—Sur les bréches osseuses et les minerais de fer
pisiforme de méme position géographique, 410 (2 plates).
—. WO NIG Sgig) hsp

Tournal.—Sur la constitution géognostique du bassin et des environs
de Narbonne, 19.

Ad. Brongniart.—Sur les plantes fossiles d’Armissan, 48 (plate).

Goldfuss.—Sur la place qu’occupent les trilobites dans le régne animal,
83 (plate).

Jeeger.—Sur les plantes fossiles du grés de construction de Stuttgart,
92

Marcel de Serres.—Sur les Arachnides et les Insectes fossiles, 98.
Cuvier.—Sur un ouvrage de MM. Croiset et Jobert, intitulé—
““ Recherches sur les Ossemens fossiles du Puy-de-Dome,” 218.
Ad. Brongniart.—Considérations générales sur la nature de la Végé-
tation qui couvrait la surface de la terre aux diverses périodes de
la formation de son écorce, 225.

Tournal.—Sur la caverne de Bize prés Narbonne, 248.

G. P. Deshayes.—Sur la famille des Rudistes, 258.

EK. de Beaumont.—Sur un gisement de végétaux fossiles et de gra-
phite, situé au col du Chardonet, 353 (plate).

A. Leufroy.—Sur une nouvelle espéce d’Hélice fossile, 405.

——. Sur une nouvelle espéce de coquille fossile du genre Férussine
(Grateloup), Stophostome (Deshayes), 401 (plate).

Dubuisson.—Sur le séléniure de cuivre trouvé en Amérique dans les
mines, dites d'argent, de Santa-Rosa, a quatre lieues d’Iguique, 408.

F. Dujardin.—Sur les terrains tertiaires de la Touraine, 412.

De Laizer.—Sur existence d’ossemens fossiles dans le tuf ou pépé-
rino d’Auverene, 415.

Sur le dusodile découvert en Auvergne, 420. _

G. P. Deshayes.—Sur le genre Podopside, 427.

Ad. Brongniart.—Hssai d’une Flore du grés bigarré, 455 (6 plates).

—. —. Vol. xvi. 1829.

Rang.—Description de cing espéces de coquilles fossiles appartenant
a la classe des Ptéropodes, 492 (plate).

Alex. Brongniart.—Observations additionelles & la notice sur les
minerais de fer pisiforme de position analogue a celle des bréches
osseuses, 89.

Necker-Saussure.—Sur les bréches en méme temps osseuses et ferru-
gineuses des mines de fer de la Carniole, 91.

F, Dujardin.—Sur les Poudingues qui surmontent la craie grossiére -.
en Touraine, 112.

See es ee géognostique sur une partie des environs d’Aix,

3.

DONATIONS. 625

Annales des Sciences Naturelles. Zoologie. Vol. xvi. (continued).

H. de Villeneuve.—Sur les terrains houillers et sur les calcaires qui
leur sont inférieurs en Belgique, 162.

J. Desnoyers.—Sur un ensemble de dépdts marins plus récens que les
terrains tertiaires du bassin de la Seine, et constituant une for-
mation distincte, 171, 402.

Marcel de Serres.—Sur les circonstances qui paraissent avoir accom-
pagné le dépdt des terrains tertiaires, 145.

De Bonnard.—Sur les gites de manganése de Romanéche, 285,

. Vol. xvii, 1829.

P. Roux.—Description d’une nouvelle espéce de crustacé fossile, 84

late).

pee e Jobert.—Sur une machoire d’ Antracothernun trouvée dans
les grés tertiaires de la Limagne, 139 (plate).

L. von Buch.—Sur les Ammonites, 267 (plate).

Hi. P. Boblaye——Sur la formation Jurassique dans le nord de la
France, 35.

Jobert.—Sur quelques points de la Géologie de l’Auvergne, 89.

Cassas.—Sur le tremblement de terre des environs d’ Alicante, 105.

Dufrénoy.—Des Formations jurassiques dans le sud-ouest de la
France, 192 (plate).

H. de Beaumont.—Note sur l’uniformité qui regne dans la consti-
tution de la ceinture jurassique du grand bassin géologique qui
comprend Londres et Paris, 254.

Marcel de Serres et Farines.—Sur la caverne a ossemens d’Argou, 276.

H. T. De la Beche.—Note sur les différences soit primitives, soit pos-
térieures au dérangement des couches, qu’on peut observer dans les
roches stratifiées, particuliérement dans celles qui sont supérieures
au grés rouge, 426.

Van Breda et Van Hees.—Sur des dents de Ruminans, de Pachy-
dermes et de Carnassiers, trouvées dans la formation crayeuse de
la montagne de Sainte-Pierre de Maéstricht, 446.

Tournal, fils—Description d’un dépdt mixte de gypse fibreux secon-
daire et de roches pyrogénes, 457.

——. Pvol, xvii, 1.829)
L. von Buch.—Sur la distribution des Ammonites en familles, 417
(plate). '

HE. de Beaumont.—Recherches sur quelques-unes des révolutions de
la surface du globe, présentant différens exemples de coincidence
entre le redressement des couches de certains systémes de mon-
tagnes, et les changemens soudains qui ont produit les lignes de
démarcation qu’on observe entre certains étages consécutifs des
terrains de sédiment, 5, 284 (8 plates).

Rasoumovski.—Des gros blocs de roches que l’on trouve épars ou
accumulés sur des terrains de natures trés-diverses, 133.

C. Lyell et R. I. Murchison.—Sur les dépéts lacustres tertiaires du
Cantal, et leurs rapports avec les roches primordiales et volca-
niques, 172 (2 plates).

Jobert.—Sur la division des terrains en un grand nombre de couches

de différente nature, 225 (plate).

Tournal.—Considérations théoriques sur les cavernes 4 ossemens de
Bize, prés Narbonne (Aude), et sur les ossemens humains confon-

dus avec des restes d’animaux appartenant 4 des espéces perdues,
242, oe | E

626 DONATIONS.

Annales des Sciences Naturelles. Zoologie. Vol. xviii. (continued).

LL. von Buch.—Carte géologique du terrain entre le lac d’Orta et
celui de Lugano, 258 (plate).

i. de Beaumont.—Sur la forme la plus ordinaire des objections rela-
tives a Vorigine attribuée 4 la Dolomie, 269.

Naudot.—Sur les os fossiles de Paleotheriwm, de Lophiodon et de
Crocodiles, découverts 4 Provins, dans un banc régulier de calcaire
lacustre, 426 (2 plates).

A. G. Kupfer.—Essai d’un tableau géognostique de l’Oural, 441. -

Voli mx 330:

i. de Beaumont.—Sur quelques-unes des révolutions de la surface
du globe, &c., 5, 177 (2 plates).

Rozet.—Notice géognostique sur quelques parties du département
des Ardennes et de la Belgique, 115 (plate).

Alex. Brongniart.—Sur deux mémoires de M. Virlet, relatifs a la
Géologie de la Messénie, et notamment a celle des environs de
Modon et de Navarin, 259.

E. de Beaumont.—Sur les formes et les relations des Volcans, d’aprés
M. Léopold von Buch, et particuliérement d’aprés sa description
physique des iles Canaries, 390 (2 plates).

De Gasparin.—Sur la formation d’un lac dans le département de la
Droéme, 424.

ee POL. Kexeen eSOy

Cauchy, Sauveur, et d’Omalius d’Halloy.—Sur les mémoires pré-
sentés en réponse a la question relative a la constitution géologique
de la province de Liége, 52.

Marcel de Serres.—Sur les rapports qui semblent exister entre la
disposition générale des anciens bassins marins littoraux, et la
nature des dépots tertiaires que l’on y observe, 65.

J. D. Godmann.—Description d’un nouveau genre de quadrupédes
mammiferes fossiles, 292 (plate).

Ad. Brongniart.—Sur la composition de Vatmosphére a diverses
époques de la formation de la terre, 427.

——. ——. Vol. xxi. 1830,
P. Savi—Sur la bréche de wake et de calcaire appelée “ Mischio di
Serravezza,” 68.
H. de Beaumont.—Sur la direction et l’age relatif des montagnes ser-
pentineuses de la Ligurie, 418.

ee ol xc eee ie

E. de Beaumont.—Sur les rapports qui existent entre le relief du scl
de l’ile de Ceylan et celui de certaines masses de montagnes qu’on
apercoit sur la surface de la Lune, 88 (plate). ;

. Sur les observations faites par M. Rozet dans les montagnes
du nord de P Afrique, 110.

Boblaye.—Sur la constitution géologique de la Morée, 115 (plate).

E. de Beaumont.—Sur un travail de M. Conybeare, intitulé “ Examen
de ceux des phénoménes géologiques qui touchent de plus prés aux
spéculations théoriques,”’ 173.

Kupffer.—Observations géognostiques faites pendant un voyage dans
les environs du mont Hlbronz, dans le Caucase, 239.

Rozet.—Notice géologique sur les environs d’Alger, 318.

Alex. Brongniart—Sur un mémoire de M. Dufrénoy, ayant pour titre
“Des caractéres particuliers que présente le terrain de craie dans
le sud de la France et sur les pentes des Pyrénées,” 436 (plate).

—

DONATIONS. 627

Annales des Sciences Naturelles. Zoologie. Vol. xxii. 1881.

Alex. Brongniart.—Sur les orbicules siliceux et sur les formes & sur-
faces courbes qu’affectent les agates et les autres silex, 166.

—— MNO. KRIV whoo,

-C. Prévost.—Sur le nouvel ilot voleanique de la mer de Sicile, 108.
Cuvier.—Sur un travail de M. Deshayes ayant pour titre “ Tableaux
comparatifs des coquilles vivantes avec les fossiles des terrains ter-
tiaires de l'Europe,” 176.
Dufrénoy.—Sur la position géologique du calcaire de la Brie, et en
particulier sur celui des environs de Champigny, 240.
Reboul.—Sur la structure des Pyrénées, 253.
Roulin.—Sur une Emeraude gigantesque, 260.
Cuvier.—Analyse des travaux de l’Académie des Sciences,—Minéra-
logie et géologie, 184.
Beudant.—Sur l’ Histoire des Végétaux fossiles publiée par M. Adolphe
Brongniart, 455.

Wol. xxv.) L632.

Dufrénoy.—Sur les diverses époques de soulévement de la chaine des
Pyrénées, 88.

T. Christie.—Sur certains dépots récens de la Sicile et sur les phéno-
meénes relatifs a leur élévation, 164 (2 plates).

Pentland.—Note contenant la détermination des ossemens fossiles des
cavernes voisines de Palerme, 208.

Rozet.—Note sur la géologie des environs d’Alger, 214.

Hi. de Beaumont.—Fraemens géologiques tirés de Stenon, de Strabon
et du Boun-Dehesch, 537.

Vol. xxvi. 1832.

G. Rose.—Réunion du Pyroxéne et de l’Amphibole en une soule
espéce minérale, 90.

HK. de Beaumont.—lragmens géologiques tirés de Stenon, de Kazwini
et du Boun-Dehesch, 565.

Lesauvage.—Sur le genre de Polypier fossile, Thamnastérie, 328
(plate).

pee
.

Voll xxvii. . 1832.

Dufrénoy.—De la relation des Ophites, des Gypses et des sources
salées des Pyrénées, et l’époque 4 laquelle remonte leur apparition,
170.

Chaudruc de Crozannes.—Sur un mémoire par M. Girard relatif 4 des
dépots d’Huitres dans le département de la Charente-Inférieure,

J. Dumas.—Sur un mémoire de M. H. Gaultier de Claubry, sur les
calcaires nitrifiables des environs de Paris, 448.

ee Vol, xxvill. 183d.

Dufrénoy.—Sur la position géologique du marbre Campan, 181.

H. de Thury.—Sur les cavernes calcaires de Cusy, dans les Beauges,
et sur les sables auriféres et gemmiféres du Chéran, en Savoie, 344.

A. Brongniart.—Sur les travaux géologiques de M. C, Gay, 394.

—. molec, _ 1833.

L. yon Buch.—Sur les Ammonites et leur distribution en familles ;
sur les espéces qui appartiennent aux terrains les plus anciens, et
sur les Goniatites en particulier, 5, 45 (6 plates).

—_—

628 DONATIONS.

Annales des Sciences Naturelles. Zoologie. Vol. xxx. 1833.

Ad. Brongniart.—Sur un Conifére fossile du terrain d’eau douce de
Vile d’Ileodroma, 168.

Dufrénoy.—Sur le gisement de la mine de fer de Rancée et sur le
terrain dans lequel elle est enclavée, 59.

Virlet.—Notes géologiques sur les iles du nord de la Gréce, et en
particulier sur un terrain de calcaire d’eau douce 4 lignites, 160,

——. Revue Bibliographique. 1829-381.

Annales des Sciences Naturelles. Zoologie. 2°Série. Vol.i. 1834,

Cuvier’s ‘ Recherches sur les ossemens fossiles,’ noticed, 255.

Alex. Brongniart et F. Cuvier.—Sur un mémoire de M. Christol,
ayant pour objet de ramener au genre Dugong les débris fossiles
que M. G. Cuvier avait rapprochés des Hippopotames, 282,

—. Vol.u. 1834.

G. A. Mantell.—Sur la découverte des ossemens fossiles de ’Zgua-
nodon, dans la formation de Glauconie sableuse (Lower Greensand),
63.

G. de Munster.—Sur les Clyménes et les G'onvatites du calcaire de
transition du Fichtelgebirge, 65 (6 plates).

Vol. am) 1835,

Gaillardot.—Sur les fossiles du calcaire conchylien de la Loraine,
extraites d’une lettre adressé aux redacteurs, 46.
L. von Buch.—Sur les Huitres, les Gryphées, et les Exogyres, 296.

Viol.tv. ~lss5:

De Christol.—Sur les caractéres des grandes espéces de Rhinocéros
fossiles, 44 (2 plates).

De Humboldt.—Sur des empreintes de pieds d’un quadrupéde dans la
formation de grés bigarré de Hildburghausen en Allemagne, 135

late). ie

fro des traces de pattes d’animaux inconnus contre-épreuvées
dans le grés, prés de Hildburghausen, 139.

De Christol.—Comparaison de la population contemporaine des Mam-
miféres de deux bassins tertiaires du département de ’Hérault, 193
(2 plates).

————

———

ee

eee

Vol v. 1830.

Blainville-—Sur le empreintes trouvées dans grés bigarré, 317.

Deshayes.—Sur la température des périodes tertiaires en Hurope
Waprés la distribution des coquilles fossiles, 289.

Falconer et Cautley—Sur le Sivatherium gigantewm, nouveau genre
de Ruminant fossile, 348 (plate).

Hitcheock.—Sur des empreintes de pieds d’oiseaux dans le grés rouge
de Massachusets, 154, 206.

Flourens.—Sur une téte d’ours fossile, 224.

uo Niol.evL visas

Deshayes.—Sur les “ Observations générales sur le genre Belemnite,”
par M. de Blainville, 354.

Milne-Hdwards.—Sur un nouveau genre de Polypiers fossiles nommé
Mélicérite, 345.

SS

DONATIONS. 629

Annales des Sciences Naturelles. Zoologie. 2° Série. Vol. vi. (con-
tunued).

Dujardin.—Sur les Polypiers fossiles de la Craie, 319.

Alex. Brongniart.—Sur l’existence de fossiles microscopiques dans les
roches en apparence homogénes, 56, :

D’Orbigny.—Sur des ossemens fossiles découverts dans une assise
nouvelle de l’argile plastique du bassin de Paris, 126.

Ehrenberg.—Sur l’existence d’Infusoires fossiles et sur leur profusion
dans la nature, 231 (plate).

Kaup.—Sur le Dinothervum, 124. .

Duvernoy.—Sur quelques fossiles de l’Alsace et du Jura, 252.

De Blainyille.—Sur une téte de chameau fossile trouvée dans le grés
du Sous-Hymalaia, 317.

Milne-Edwards.—Sur les Polypiers fossiles du genre Eschare, 321
(4 plates).

Wola 2857.

Cautley et Falconer.—Sur les animaux fossiles découverts dans les
couches supérieures des dépots tertiaires des montagnes Sivalek de
V’Himalaya, 60.

Baker.—Sur le chameau fossile du Sub-Himalaya, 62.

Lartet.—Sur les ossemens fossiles des terrains tertiaires de Simorre,
de Sansan, &c., dans le département du Gers, et sur la découverte
récente d’une machoire de singe fossile, 116.

Sur les ossemens fossiles trouvés dans le département du Gers,

122.

De Blainville.—Sur la découverte de plusieurs ossemens fossiles de
quadrumanes daus le dépot tertiaire de Sansan, prés d’Auch, 282.
H. Milne-Edwards.—Sur une bréche osseuse située entre Oran et

Mers-el-Kebir, 216,
Baker et Durand.—Sur la machoire fossile d’un quadrumane qui se
rapproche des genres Semnopithéque et Cynecéphale, 370.
Eudes Deslongchamps.—Sur le Pekilopleuron Bucklandi, grand Sau-
rien fossile intermédiaire entre les Crocodiles et les Lézards, 255.
Darwin.—Sur la découverte de quelques ossemens fossiles et sur leur
profusion dans la nature, 27. /

Turpin.—Analyse ou étude microscopique des différens corps orga-
nisés et autres corps de nature diverse, qui peuvent, accidentelle-
ment, se trouver enveloppés dans la pate translucide des silex, 129,

———, : we Vol vie | Tear

Jourdan.—Sur un rongeur fossile d’eau douce du centre de la France,
considéré comme un type générique nouveau, le genre Theridomys,
127, :

Falconer et Cautley—Sur la découverte de deux nouvelles espéces
de Quadrumanes fossiles, 255.

Serres.—Sur une Argonaute fossile, 128,

Volv ix. 11838;

Owen.—Sur le crane du Zoxodon Platinses, grand mammifere perdu
que l’on doit rapporter a l’ordre des Pachydermes, mais qui offic en
méme temps des affinités avec les Rongeurs, les Edentés et les
Cétacés herbivores, 25 (plate).

Marcel de Serres.—Sur les animaux des terrains tertiaires marins
supérieurs découverts dans le sol immergé des environs de Mont-
pellier, 380,

—————_

630 DONATIONS.

Annales des Sciences Naturelles. Zoologie, 2° Série. Vol. ix. (con-
tinued).

Marcel de Serres. Sur les cavernes 4 ossemens, 380.

H. oan Meyer.—Sur les ossemens fossiles du grés bigarré de Soultz-
les-Bains, 376.

Milne-Edwards.—Sur les Crisies, les Hornéres et plusieurs autres
Polypes vivans ou fossiles, dont Vorganisation est analogue a celle
des Tubulipores, 193 (6 plates).

Wolex 1338.
De Laizer et De Parieu.—Sur un nouveau genre de Pachyderme fossile,
539 (plate).

Beyrich.—Sur les Goniatites qui se trouvent dans les terrains de tran-
sition du Rhin, 65 (2 plates).

—

Wolh xi els3o:

De Laizer.—Sur la machoire d’un Carnassier fossile, nommé Hyenodon
leptorhynchus, 27.

De Blainville.—Sur l’ancienneté des Edentés 4 la surface de la terre,
113.

Lund.—Sur les Mammiféres fossiles du Brésil, 214.

Necker.—Sur la nature minéralogique des Coquilles, 52.

= Wales, ISSo.

R. Owen.—Description d’une dent et d’une portion de squelette du
Glyptodon, 156.

Lund.—Sur la Faune fossile du Brésil, 205.

Harlan.—Sur le Basilosaure et le Batrachiosaure, 221.

F, Dujardin.—Sur une téte fossile d’ Hyenodon trouvée au bord du
Tarn, prés de Rabasteins, 379.

Vol. xi. 1840.

Lecoq.—Notice sur les travaux de M. Voltz, 348.
Lucas.—Nouvelle espéce de Crustacé fossile, 63.
Lund.—Nouvelles recherches sur la Faune fossile du Brésil 310.
Ouchakeff—Sur un Termes fossile, 204.

Voltz.—Sur le genre Actinocamax, 354.

Volwesive S0;

Marcel de Serres.—Description de quelques fossiles nouveaux (genres
Tysoa et Nisea) du midi de la France, 5 (2 plates).

——, Vol. xy. 1841.

Christol.—Sur divers ossemens fossiles attribués par Cuvier 4 deux
Phoques, &c., et rapportés au Metaxrytherium, nouveau genre de
Cétacé, 307 (plate).

Volexv., al S4alk

Edwards (H. Milne).—Rapport sur un mémoire de M. Duval relatif
aux Lelemnites des terrains cretacés inférieurs des environs de
Castellane, 281.

Marcel de Serres,—Sur la découverte d’un squelette entier de Metary-
thervum, 24,

Se annem

eee

————

ae

DONATIONS. 631

Annales des Sciences Naturelles. Zoologie. 2° Série. Vol. xvi. (con-
Daud).
D’Orbigny (Alcide).—Considérations paléontologiques et géographi-
ques sur les Céphalopodes acétabuliferes, 17.
—. Considérations zoologiques et géologico-géographiques sur les
Ammonites du terrain crétacé, 113, ;

: Vol. xvii. 1842.

D'Orbigny.—Considérations zoologiques et géologiques sur les Ru-
distes, 173.

Considérations sur les Céphalopodes des terrains cretacés, 230.

——. Mémoire sur deux genres nouveaux de Céphalopodes fossiles,
362 (2 plates).

Eschricht.—Nouvelles remarques sur le Diceras, 379.

ee

Vol. xviii. 1842.

- Bouchard-Chantereaux.—Sur le genre Productus, 158 (plate).
D’Orbigny.—Mémoire sur les Bélemnites, 241.

Vol.xaxey 1643:

D’Orbigny.—Sur la paléontologie de l’Amérique méridionale, com-
parée a la paléontologie EKuropéenne, 263.

Owen.—Description du squelette d’un paresseux gigantesque fossile
(le Mylodon robustus), 221 (plate).

—— Ce VOlaxxe . [o45:

Edwards (Milne-).—Sur deux Crustacés fossiles de l’ordre des Iso-
podes, 326.

Marcel de Serres.—Sur les grandes Huitres fossiles des terrains ter-
tiaires des bords de la Méditerranée, 142 (2 plates).

D’Orbigny, A.—Sur l’ensemble des Gastéropodes des terrains cré-
tacés, 26.

—_—_——
t

3° Serie. Vol. i. 1844.
Duvyernoy.—Sur une machoire de Girafe fossile découverte 4 Issou-
dun, 36 (plate).

Owen.—Sur des ossements fossiles d’un animal gigantesque de la
famille des Autruches, 188.

Valenciennes.—Description de quelques dents fossiles de poissons,
trouvés aux environs de Staoueli (Alger), 99 (plate).

——. Vol.u. 1844.

Agassiz.—Sur la succession des poissons fossiles dans la série deg for-
mations eéologiques, 251.

Marcel de Serres.—Sur les terrains d’eau douce du bassin emergé de
Castelnaudary: Coguilles, 168 (plate).

——. Voli. 1845.

Agassiz.—Sur les poissons fossiles de l’argile de Londres, 21.
Cautley et Falconer.—Sur le Colossochelys atlas, tortue fossile gigan-
tesque découverte dans l’Inde, 190.
D’Orbigny.—Sur les lois qui président a la distribution géographique
des mollusques cétiers marins, 193,
VOL, XXII,—PART I, } 2U

632 DONATIONS,

Annales des Sciences Naturelles. Zoologie. 3°Série. Vol. iv. 1845.

Forbes.—Sur la distribution topographique des Mollusques marins
17 .
Marcel de Serres.—Sur les fossiles du bassin d’Aix, 249,

—. ——, - Vol.v. 1846,

Gervais (Paul).—Sur diverses espéces de Mammiféres fossiles du midi
de la France, 248. * pei
Mammiferes fossiles de Vaucluse, 257.

——. Mammiféres fossiles de l’Hérault, 263.
—— et Marcel de Serres.—Mammiféres fossiles de ’Hérault, 266.
Owen.—Description de quelques cranes fossiles trouvés par M. Bain
dans une couche de grés 4 l’extrémité sud-est de Afrique, et con-
stituant un nouveau genre de Reptiles (le Dicynodon), dans Vordre
des Sauriens, 271.

. ._ Vol. vi. 1846,

Agassiz et Desor.—Catalogue raisonné des familles, des genres et des
espéces de la classe des Hchinodermes, 305 (2 plates).

Vol. vii. 1847.

Agassiz et Desor.—Catalogue raisonné des Echinides, 129.
Marcel de Serres et Figuier.—Sur la pétrification des coquilles dans
la Méditerranée, 21. -

é Vol. vii. 1847.

Agassiz et Desor.—Catalogue raisonné des Echinides, 5, 355.

P. Gervais.—Surles Mammiféres fossiles du midi de la France, 203.

et Marcel de Serres.—Sur les Mammiféres dont on trouve les
restes fossiles dans les sables marins de Montpellier, 224.

Alcide D’Orbigny.—Considérations zoologiques et géologiques sur
les Brachiopodes, 241 (plate).

5 Vol. ix. 1848.

Milne-Edwards et Haime.—Sur la structure et le developpement des
polypiers en général, 37 (3 plates). 7

Monographie des Turbinolides, 211 (4 plates).

: . ——, Vol.x. 1848.

Milne-Edwardset Haime.—Monoeraphie des Eupsammides, 65 (plate).

——. Monographie des Astréides, 224 (5 plates).

Vol. xi. 1849. i

~_- Milne-Edwards. et Haime.—Monographie des Astréines, 235,

=, Vol, xm. . [edo:

Bouchard-Chantereaux.—Sur un nouveau genre de Brachiopode (le
Dandsoma), 84 (plate).

Milne-Edwards et Haime.—Monographie des Astréides, 95, -

... Discours nécrologique sur M. de Blainville, 375. 7

Haime.—Sur la Jinia, nouveau genre de l’ordre des Hchinides, 217
(plate).

Owe ee la Scolicia prisca, annélide fossile de la craie, 265.

—, ——. 4°Série. Vol vy. 1856.

Se

DONATIONS, 633

Annales des Sciences Naturelles. Zoologie 4° Série, Vol. vi. 1856.

Hébert.—Sur la faune des premiers sédiments tertiaires parisiens
(Mammiféres, Pachydermes, du genre Coryphodon), 87 (2 plates).

— : wa VOL yt Tepe.

Blanchard.—De la détermination de quelques oiseaux fossiles et des
caractéres ostéologiques des Gallides, 91 (3 plates). BRS |

Vol. vii. 1857.

Marcel de Serres.—Sur les altérations des coquilles des mollusques
Lamellibranches et Gastéropodes, 377.

Vol,ix, E658.

Beaumont, Elie de.—Sur un nouveau gisement des fossiles découvert
derniérement en Angleterre, 318.

Delbos.—Sur les ossements des cavernes de Sentheim (Haut-Rhin),
précédées d’observations sur l’ostéologie de l’ours brun des Pyré-
nées, 195,

Falconer.—Sur deux nouvelles espéces de Mammiféres fossiles trou-
vées dans l’oolite de Purbeck, et appartenant au genre Plagiaulaz,
317.

——., : Pie VOln x) Losey

Salter.—Sur l’existence d’un poisson fossile dans la couche inférieure
des roches de Ludlow, 342.

a Ol xt, Looe

Vol. xii. 1859.

Marcel de Serres.—Sur les modifications que les coquilles éprouvent
et qui ne dependent d’aucune affection morbide, 377,

Vol; xin* “1860:

Delbos, J.—Sur les ossements des carnassiers des cavernes de Sentheim
(Haut-Rhin), 47.

Marcel de Serres.—Des espéces perdus et des races qui ont disparu
des lieux qu’elles habitaient primitivement, 297.

Volcxtv. | 1860:

Delbos, J.—Sur les ossements des carnassiers fossiles des cavernes de
Sentheim, 5.

Edwards (Alphonse).—Histoire des crustacés Podophthalmaires fos-
siles, 129 (10 plates).

Monographie des Thalassiniens fossiles,-295 (6 plates).

Lartét.—Sur Vancienneté géologique de l’espéce humaine dans )’Eu-
rope centrale, 117.

ee — — —, )S Vol, xv... 18S6L

-Gaudry.—Comptes rendus des fouilles executées en Gréce sous les
auspices de l’Académie des Sciences, 159.

Lartét.—Sur la coexistence de Homme et des grands Mammiféres
fossiles réputés caractéristiques de la derniére période géologique,
139 (4 plates).

Morch.—Sur le Jélin d’Adanson et sur le genre Pleurodictyum de
Goldfuss, 369.

‘Valenciennes.—Sur les collections de Mammiféres fossiles, recueillis
par M. Gaudry 4 Pikermi, prés d’Athens, 117. :

. 2u2

os

rs

. nena ene
°

ee
.

oe
e

er -__oO,

634. DONATIONS.

Annales des Sciences Naturelles. Zoologie. 4° Série. Vol. xvi. 1861.

Gervais.—Sur différentes espéces de Vertébrés fossiles observés pour
la plupart dans le midi de la France, 288.

Jourdan.—Description des restes fossiles de deux grands Mammiféres
constituant les genres Riizoprion et Dinocyon, 369 (plate).

Wol. xv. 1862.

Alphonse Milne-Edwards.—De Vexistence de Vhomme pendant la
période quaternaire dans la grotte de Lourdes, 227 (plate).

Lubbock.—Recherches géologico-archéologiques récentes faites en
Denmark sur les Kjokkenmoddings, 273 (plate).

Sur les anciennes habitations lacustres de la Suisse, 295.

Se Wola xem ISO

Mayer.—Sur la découverte d’un Vertébré muni de plumes dans un
dépét de I’époque jurassique, 341.

Alphonse Milne-Edwards.—Monographie des Crustacés fossiles de
la famille des Cancériens, 30 (10 plates).

Van Breda.—Sur les haches d’Amiens et d’Abbeville et les dents de
mammiféres de Maestricht, 336.

ee oleae enlic@on

Pe Re eB OIA ees | JUSS.

Milne-Edwards (Alphonse).—Sur la distribution péognapialan des
oiseaux fossiles, et description de quelques espéces nouy elles, 133
(plate).

——. Monographie des Crustacés fossiles de la famille Cancériens,
293 (9 plates).

Annals and Magazine of Natural History. Third Series. Vol. xvii.
Nos. 100- 102. April to June 1866.

P. P. Carpenter.—Pleistocene Fossils collected by Col. E. Jewett at
Sta. Barbara, California, 274.

W. B. Carpenter.—Rhynchonella Gemitziana, 306.

H. Seeley.—Epitome of the Evidence that Pterodactyles are not
Reptiles, but a new Subclass of Vertebrate Animals allied to Birds
(Saurornia), 321.

J. Nicol’s ‘Geology and Scenery of the North of Scotland,’ noticed,
467.

A. Milne-Edwards.—Bones of the Dodo recently collected in the
Mauritius, 473.

Leonhard und Geinitz’s Neues Jahrbuch fiir Mineralogie, Geologie,
und Paliontologie. Jahrgang 1866. Hefte 2 & 3.

H. R. Goppert.—Beitrige zur Kenntniss fossiler Cycadeen, 129
(plate).

F, Romer.—Protolycosa anthracophila, eine fossile Spinne aus dem
Steinkohlen-Gebirge Oberschlesiens, 136 (plate).

H. B. Geinitz.—Ueber Arthropleura armata in der Steinkohlen-For-
mation von Zwickau, 144.

C. Naumann.—Ueber den Granit des Kreuzberges bei Carlsbad, 145
(plate).

Mohr.—Ueber die Natur der Silicate, 181.

HE. Haeckel.—Ueber zwei neue fossile Medusen aus der Familie der ©
Rhizostomiden, 257 (2 plates).

———d
e

nd
e

DONATIONS, 635 .

Leonhard und Geinitz’s Neues Jahrbuch ftir Mineralogie, Geologie,
und Palaontologic. Jahrgang 1866. Hefte 2 & 3 (continued).

J. v. Barrande.—Beleuchtung einiger Ansichten tber die Colonien,
293.

U. Schloenbach.—Ueber die Parallelen zwischen dem oberen Pliner .

Norddeutschlands und den gleichalterigen Bildungen im Seine-
Becken, 309.

E. Reichardt.—Das Steinsalzberewerk Stassfurt und die Vorkomm-
nisse in demselben, 321.

Letters; Notices of Books, Minerals, Geology, and Fossils, 61.

L’Institut. 1 Section. 34° Année. Nos. 1679-1690. March to
May 1866.

Paleontographica: herausgegeben von Dr. Wilh. Dunker. Vol. xiu,
Lief. 5. March 1866.
F, A. Rémer.—Beitrige zur geologischen Kenntniss des Norddeut-

schen Harzgebirges, 201 (8 plates).
D. Brauns.—Der Sandstein bei Seinstedt unweit des Fallsteins, 239

(plate).

“eae herausgegeben von Hermann von Mayer. Vol.
xv. Lief. 5. March 1866.

rR tri. —Corallen aus palaolitischen Has) ON x 173 (14
plates).

Vol. xv. Lief. 2. March 1866.

H. von he — Homoeosaurus Maxinuliani aus dem lithogr npbieclion
Schiefer von Kelheim, 49 (plate).

H. Hagen.—Die Neuroptera des lithographischen Schiefers in Bayern,
Part i 1., 57 (4 plates).

——. Supplement-Band. Lief. 6. March 1866.

A. Hellmann.—Die Petrefacten Thiiringens nach dem Materiale des
herzogl. Naturalien-Kabinets in Gotha, 41 (plate).

.
ee
e

Ill. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Ftalies.

Abich, H. Finleitende Grundziige der Geologie der Halbinseln
Kertsch und Tamau. 1865.

Observationes de Elasmotherii relma 1864.

Les Hydrographiques : recueil d’avis, instructions, documents,
_ et mémoires relatifs 4 Vhydrographie et 4 la navigation. 2° et 3°
Trimestres de 1865. 1865. From the Dépét de la Marine.

Australia. Supplément au Routier de l’Australie, Cote est, détroit
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Brandt, J. F. Bemerkungen iiber die Classification der kaltbliitigen
Riickenmarkthiere zur Beantwortung der Frage: Was ist ein
Fisch? 1865.

—- 636 DONATIONS,

Brandt, J. F. Bemerkungen iiber die Verbreitung und Vertilgung
' der Rhytina. 1862.

Bericht tiber die Acquisitionen der zoologischen und zooto-
mischen Sammlungen der Kaiserl. Akademie der Wissenschaften
wahrend des 1864sten Jahres und die darin ausgefihrten wissen-
schaftlichen Arbeiten. 1864.

Bericht iiber den ersten Theil meiner Beitrige zur Kenntniss
der Entwickelungsstufen der ganoiden Fischformen. 1865.

——. Bericht tiber eine Abhandlung: Untersuchung der Gattung
Hyrax in anatomischer und verwandtschaftlicher Beziehung.
1862. |

Mittheilungen iiber die Naturgeschichte des Mammuth oder
Mamont (Hlephas primigenius). 1866.

Noch einige Worte iiber die Vertilgung der Rhytina. 1865.

Rapport sur un mémoire qui, en traitant Vostéologie com-
parée de la Rhytine, constitue la seconde partie de mes Symbole
Sirenologice. 1861.

——. Ueber die bisher aufeefundenen Reste des Hlasmotherium.
1864 7

Buckman, J. Science and Practice in Farm Cultivation. 1865. -

Céntral Hall of Arts and Sciences. Lists of Patrons and Promoters,
&c. 1866. From the Royal Horticultural Society.

Costa. Instructions sur les cétes est de Chine, la mer Jaune, les
golfes de Pe-Chili et de Liau-Tung et la cote ouest de la Corée,
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Daubrée. Expériences synthétiques relatives aux Météorites, 1866.
De la Planche, H. Pilote de la Mer Noire. 1865. From the Dépét

de la Marine,
Doughty, C. M. On the Jostedal-brae Glaciers in Norway. 1866.

Duncan, P. M. The Histology of the Reproductive Organs of the
nid (Ligridia conchiflora) ; with a description of the Phenomena
of its Impregnation. 1866.

ee E. Essai d’une Carte Géologique des environs de Dinant.
1866,

——. Sur le Calcaire Carbonifére de la Belgique et du Hainaut
Francais. 1865,

Gaudry, A. Considérations générales sur les Animaux Fossiles de
Pikermi. 1866.

Cippett, .f.. Ueber die fossile Kreideflora und ihre Leitpflanzen.

DONATIONS. 637

Gras, A. le. Tustructions Nautiques sur la cote est de la Malaise,
le golfe de Siam, les cétes de la Cochinchine, le golfe de Tonquin,
et la céte sud de la Chine. 1865. From the Dépét de la Marie.

Gray, J. Biographical Notice of the Rev. David Ure; with an
_ Examination, critical and detailed, of his sneer 9 of Rutherglen:
and Hast Kilbride. 1865.

Giimbel, C. W. Ueber das Vorkommen von ZHozoon im ostbayer-
ischen Urgebirge. 1866.

Hall, T. M. The Geology of North Devon. 1866.

Hill, J. Fossils arranged according to their obvious Characters ;
with their History and Description. 1771. From W. Wihataker,
Esq., F.G.S.

Hochstetter, F. von. Ueber das Vorkommen von Hozoon im tata
limischen Kalke von Krummau im siid'chen Bohmen. 1866.

Hopkins, E. Terrestrial Magnetism with reference to the compasses |
. of Iron Ships: their “deviation” and remedies. 1866.

Industrial Resources of the Tyne, Wear, and Tees, including reports
on the local: manufactures. 1864. From John Evans, Esq.,
ERS., Sec. GS.

Jenyns, L. Phosphatic Nodules, obtained in the Eastern Counties
for Agricultural purposes. 1866.

Karrer, F. Ueber das Auftreten von Foraminiferen in den alteren
Schichten des Wiener Sandsteins. 1865.

Rotuen, A. v. Nachtrag zu dem Autsatze uber die re
Fauna. 1865.

Ueber einige Aufschliisse im Diluvium stidlich und ostlich
von Berlin, 1866,

heres, L. Note sur la découverte de ae taillés, en Syrie, accom-
pagnée de quelques remarques sur l’age des terrains a consti-
tuent la chaine du Liban. 1865.

Poteries primitives, instruments en os et silex taillés des
cayernes de la Vieille Castille (Espagne). 1866.

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Laube, G. C. Die Bivalven des braunen Jura von Balin mit Be-
ricksichtigung ihrer geognostischen Verbreitung in Frankreich,
_ England, Schwaben und anderen Landern. 1866.

Lea, I. On Leava Leidyi.

638 DONATIONS,

Lea, I. Descriptions of 14 new species of Melanide.

—. Descriptions of 11 new species of exotic Unionide.

——. Descriptions of 24 new species of Unionde.

——. Descriptions of a new species of Unio and a Monocondylea. |
—. Description of a new genus of the family Meande.

——. Descriptions of 11 new species of Melanide.

——. Description of, and remarks on Planorbis Newberry.

——. Descriptions of 6 new species of Unionide from Lake Nyassa.
———. Descriptions of 6 new species of Succinea, &c.

——. Descriptions of 13 new species of Melanide.

——. Description of a new species of Planorbis.

——. Descriptions of 5 new species of Lymmnea.

——. Descriptions of 2 new species of Unionide from South Africa.
——. Descriptions of 24 new species of Physa.

——. Descriptions of 6 new species of Western Asiatic Unionidae.

——. Descriptions of 3 new species of exotic Uniones.

——. Descriptions of 8 new species of Unio. 1866.

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Recherches sur les Chronomeétres et les Instruments Nautiques.
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DONATIONS. 639

Reuss, A. HE. Die Foraminiferen, Anthozoen, und Bryozoen des
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Die Foraminiferen und Ostracoden der Kreide am Kanara-
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1865.

Vogt, C., e B. Gastaldi. Su aleuni antichi cranii umani rinvenuti
in Italia. 1866.

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Alpen. 1866,

VOL, XXII,.— PART I, 2s

te ee ae
es

ty

Se

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON,

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

VOLUME THE TWENTY-SECOND.

1S6G.

PART II. MISCELLANEOUS.

Fe
‘
at

deme

CONTENTS OF PART IL.

Alphabetically arranged—the Names of the Authors in capital letters.

Page
Peete MOCHSTETTER On H0z00R IM. os icey sees ve oun wals ewes 16
BaRRANDE, J. Defence of the ‘“ Colonies.”—Part III. .......... 1

Bavaria, GUMBEL on the Occurrence of Eozoén in the Primary Rocks
PI REM Dh re rare sei, c ce ab Ole yoy apap e eaca ere ees 23

Biscuor, G. Elements of Chemical and Physical Geology. Vol. ii.
PET Lao hig has a os sem Ay Ss EME SCO ORE Sp 6

Brachiopods cf the St. Cassian Beds, Dr. LAuBE on the .......... 10

Briart, A., and F.-L. Corner. On the Discovery in Hainaut, be-
low the Sands referred by Dumont to the Thanet Sands, of a

coarse Limestone with a Tertiary Fauma...........c.csceeseee 11
Brunswick, Von Kornen, on the Oligocene Tertiary Beds of Helm-

DEEPER CST PAR Sete) 9) diane wom, Flac anata Wald oer a alasee alle a! AOREMOLN 17
Caverns of the Lesse, Dupont on Explorations of the.......... 25, 28
Chemical and Physical Geology, Elements of, vol. ii. 2nd edition,

PM 3 ca aon waar stuoeengioer opine WG wr ed RRS G6
Choristoceras,,. Von HAvER on, a new Genus of Cephalopods ...... 29
Colonies, BARRANDE on the Defence of the.—Part II]............. 1

Cornet, F.-L., and A. Brrart. On the Discovery in Hainaut,
below the Sands referred by Dumont to the Thanet Sands, of a
Course Wimestone with a Yertiary Mauna.......... 0.00 eei eee 11

Defence of the “Colonies,” Part iii.,by BARRANDE...... .....5+ 1

Dupont, EK. Onthe Explorations made during the Winter of 1865-

66 in the Caverns of the banks of the Lesse .................. 25
On three Caverns in the Valley of the Lesse explored dur-

meee months of March and April 186600. ... 0 0665 0. eos 28

Ber enmee seria, HOCHSRETEAR OM 13) yf bec ee ce hee nce 16
in the Primary Rocks of Eastern Bavaria, GimBrt on the

SUSTRREIRGS OLE A ge nee 25

Fossils ip the Stages G and H of BARRANDE...............00005 2,

Gasteropods of St. Cassian, LauBE on the .......... ASHE A eke 30

iv

P
Geology, Elements of, Chemical and Physical, vol. ii. 2nd edition, ag
by BISCHOR |... !5: uae hctcures maistcones beeen oe

Germany, H&BERT on the Oligocene of.:........... ike 6a tee 19
GimpBet. On the Occurrence of Kozoén in the Primary Rocks of
Hasterm Bayarla. 2 oie de ces aes bas ees oon ee 23
Haver, F. Ona New Genus of Cephalopods ..,............. aa) ee
Hésert, KE. On the Nummulitic Strata of Northern Italy and th
Alps, and.on the'Ohgocene of Germany ~...)..s.. esse
Hocusterrer. ‘On #ozoon in Austria... 5.2... . 0.) eee 16
Hungary, 8zaBo on the Geology of Tokay................cse0e 14
Italy, Prof. HEBERT, on the Nummulitic Strata of Northern ...... 19

_ Kornen, Von. On the Fauna of the Lower Oligocene Tertiary Beds
of Helmstadt, near Brunswick ..............55.5)0he

LavuBE, G. C. On the Brachiopods and other Bivalves of the St.

Cassian: Beds. cic sc csine eestaratere € otis sole be ole clare oid 10
===. On the Gasteropods ot St; Cassian = 20.00 eee ieinneie 30
Lesse, Dupont on Explorations of the Caverns of the .......... 25, 28
Marmot in Styria, Scumrpt on Remains of the...............06. 30
Nummulitic Strata of Northern Italy, Hiperr on the............ 19

Oligocene Beds of Helmstadt, near Brunswick, Von KOENEN onthe 17
Oligocene of Germany, HEBERT on the .........5..-.s.0s5 see 19

Physical Geology, BiscHoF on the Elements of Chemical and, vol. i1.
Pind ‘CCItION 5 sn 6 a aihles ns ales ews 2 ees oe oe lo

St. Cassian Beds, LauBE on the Bivalves of the .........seee0es 10

, LauBE on the Gasteropods of the ..........00005 iat 30
Scumipt, O. On Remains of the Marmot in Styria 266 eee 30
SZABO, J. On the Environs of Tokay, Hungary ...........+.0:- 14

Tertiary Limestone in Hainaut, below the Sands referred by Dumont
to the Thanet Sands, CornET and Briart on the Discovery ofa.. 11

Tokay, Hungary, 8zap6 on the Geology of............c-cssuanee 14

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

Derence of the “‘Cotontes.”—Part III. By M. J. Barranne.

[Défense des Colonies.—III. Etude générale sur nos étages G—H, avec applica-
tion spéciale aux environs de Hlubocep, prés Prague. Par J. Barrande

1865.]
Tuts last contribution from the pen of M. Barrande treats specially
of the two highest members of his “ third fauna,” which are well
developed in the typical district of Hlubocep, and are subdivided by
the author as follows :—

metres.
h3. Soft grey and greenish shales............ccecsesesresees 20-40
h 2. a Ngee: with thin bands of impure sand-
EM SHUI ens onle aces 6as sais condabesCavecsnauhinoomisrs vcmad 150-200
Al. oe coloured highly fossiliferous shales, with
a few calcareous bands at the base ............06 20-60
g 3. Compacted nodular limestone ........00.....sssesee 00 50-100
G4 g2. Shales containing thin layers of calcareous nodules 20-150
@ C Bods of nodular limestone .....0.1.....-ccecsvescseseces 150-200

The lowest division of g rests conformably on F, the passage from
the one member to the other being gradual. Between g 1 and g 2
there nowhere exists any strongly marked line of separation; on the
contrary, the transition takes place by repeated alternations of thin
bands of limestone and beds of shale, the former diminishing in
thickness as we ascend to higher levels, while the intervening beds of
shale become progressively thicker. Towards the central portion of
g 2 the nodular limestone bands are reduced to a few subregular
layers, or are altogether absent. The passage into the overlying g 3
is equally gradual. Thin bands of yellow and red nodular limestone
separate the shales towards the highest part of this division, and be-
coming more and more numerous as we ascend, finally become pre-
dominant, and are succeeded by the compacted nodular limestone
beds g3. ‘This latter resembles precisely the lower bed g 1, but
differs widely inthe species and relative number of its organic re-
mains. In the vicinity of Chotecz and Hinter Kopanina g 2 con-
tains beds of trap-rock interstratified with the shales.

Between g3 and hf 1 the transition is more marked, although at
Hortin and near Holin there is an apparent alternation of the higher
beds of the one with the lower beds of the other. In some localities,
however, as in the valley of Srbsko, the shales of h 1 abut against the ©
higher limestone of G. Nevertheless M. Barrande is unwilling to
admit that there exists a real unconformability between the two

VOL. XXII.—PART II. B

2 GEOLOGICAL MEMOIRS.

members, and endeavours to explain away the discordance by the
supposed effects of denudation and subsequent change of position
(p. 19). The two higher members of H rest conformably on the
lower one. They are entirely unfossiliferous, with the exception of
a few fucoidal impressions on the surfaces of the sandstones which
characterize the middle division.

Of the rich fauna contained in these two zones in olen
amounting altogether to 254 species, a very small number only are
known to Britain. The fish-remains referred to the genera Cocco-
steus, Asterolepis, Gompholepis, and Ctenacanthus, which occur in g 1,
are all absent from British Silurian strata. Coccosteus first appears
in zone I’, but the species does not pass up. Hence vertebrate genera
which characterize our Old Red Sandstone series, in Bohemia occur
many hundred feet lower down in the geological scale.

As regards the Invertebrata the general results are given in the
following Table :—

General Table of the Vertical Distribution of the Fossils in the
Stages G and H.

Total

number
Genera G. Bes Species common to of io
and EF. Poe
species. ane
rom
G19? | G34 | h?| h3 gt & 97.19? & #9 &G.1G&H.| GH.
IBISHeS ay sc ueccne. ec FECES ae ae . ae a fits
Crustacea ...... 3/18) 49) 5) 2) 2)... 2 1 2 2 Vi
Cephalopoda...|15) 7} 39} 8/62) 5)... 5 2 4 4 13
Pteropoda ...... 1; 3) 10) 3} 2) 2)... 2 2 2 2 6
Gasteropoda ...| 2} 5) 16} 3) 2)...).. l 1 0 0 2
Brachiopoda ...| 8/20} 29} 8) 5) 2).. 7 3 2 2 12
Acephala ...... tS) Ola Sito) Ale 1 0 4 il 6
adiavale.seecee Lal cee CO RAEI RRE eater ee 2 0 1 0 3
301561170139/79|15 at |. 9 |) 155) ae es
303

The total number of species in the two stages G and H is there-
fore 303, which, deducting 49 for recurrent species, leaves 254 for
the entire fauna. Of the 15 species which occur in H, there are
only 4, namely, Orthoceras equisetum, Barr., Avicula consanguis,
Barr., A. rarissuma, Barr., and Cardiola retrostriata, V. Buch, which
are not contained in G. The latter, however, occurs in E.

56 species pass up from stage F, and 30 from stage K. Of these
86 species, 12 are common to both these stages, leaving 74 species, or
one-third nearly, as common to the two upper and two lower zones
of the third fauna.

gland g 3 are undistinguishable lithologically, but are easily re-
cognized by the difference in their paleontologieal contents, all

BARRANDE—COLONIES. 3

the classes, except the Cephalopods, being largely represented in g 1,
while the Cephalopods are more numerous in g 3, in the proportion
of 3 to 2 (p. 54).

g2 and h 1 may be similarly distinguished. The two beds toge-
ther contain 54 species. Of these, about 16 species occur in the
lower beds which do not occur in the higher, while the higher con-
tain two species only which are not found in the lower. The two
highest members of H are unfossiliferous and are not therefore lable
to be confounded with the shale below.

Comparing the Silurian system of Bohemia with that of England,
M. Barrande finds that. while a complete correspondence exists be-
tween the grand divisions, it does not extend to the minor ones.
Thus the fossils which characterize the Upper Silurian system of Eng-
land and the “ third fauna” of Bohemia, considered as a whole, con-
stitute one and the same general fauna, which, at its commencement,
presented very close relationship, but which, from local or other causes,
underwent in each country a different evolution, and hence that the
different zones in the two countries as distinguished by their fossils
are merely local subdivisions which have no correspondence, although
comprised in the same period of time during which the Silurian sy-
stem was being deposited. Thus we find that of the 2000 species
which characterize the third fauna of Bohemia and the 500 in England
there are only 57 species in common, 32 of which had existed previ-
ously in British Lower Silurian rocks, although some of them do not
appear in the second fauna in Bohemia. Of these 57 species, 50
oceur in the Wenlock, and 27 in the Ludlow rocks, and one passes
up into the passage-beds. In Bohemia 51 of these 57 species are
2 oe in stage E, 12 in stage F (7 being recurrent species), 5 in stage

G (4 being recurrent species), and 1 in iy it (Lingula aed
(pp. 175 & 176).

It appears, therefore, that, abstracting the passage-beds, the agen
Silurian fauna of England i is sufficiently (maniere satisfaisante) re-
presented in the stage E of Bohemia, and that stages F, G, and H of
the Prague Basin, and especially the two last, are not certainly present
in England (p. 17 gt

To render this more clear it may be well to state that the chief
palzontological characters of G are (1) the predominance of Trilobites,
and especially of Dalmanites and Bronteus, and the presence of Caly-
mene in the horizon of g1; (2) the reappearance of Cephalopods of
the genera Phragmoceras and Gomphoceras in g 3, which had disap-
peared at the close of stage E ; (3) the appearance of Gonatites, rela-
tively considerable, analogous to those of the Devonian system which
had already been ushered in by some rare forms in stage F; (4) the
sporadic appearance of Coccosteus and Asterolepis*, hitherto generally
considered as exclusively proper to the Devonian period. These
elements are entirely wanting in England, not only in the Wenlock
and Ludlow rocks, but even in the passage-beds. If, therefore, we
give to paleontological evidence the value we have hitherto attributed
to it in the classification of deposits, and above all in the comparison ©

* Carboniferous?
B 2»

4 GEOLOGICAL MEMOIRS.

of basins geographically separated, it is evident that in England
there is no distinct subdivision which can be considered as especially
the stage G of Bohemia; and the same remark is applicable to stage
H, of which the fauna is but a feeble continuation of that of G.

In Russia and the Baltic provinces the progress of discovery has
confirmed the equivalence, already laid down in 1845 by Sir R.
Murchison, between the Silurian rocks of the Isle of Oesel and those
of England; but Dr. Schmidt remarks that the subdivisions of the
Ludlow rocks cannot be recognized in the upper zones of the Island
of Oesel, and it is important to observe that of the 43 species of fish
belonging to this zone, 12 of them, among which Pterichthys [ Astero-
lepis| occurs at Ohhesaare-Pank associated with Phacops Down-
mgue, Calymene Blumenbachi, Orthoceras bullatum, O. trocheale, Car-
duola interrupta, Fterinea retrofleca, Retzia Salteri, Strophomena
filosa, Chonetes lata, and other Wenlock and Ludlow fossils, showing
as remarked by M. Barrande, that the presence of fish-remains by no
means vitiates the Silurian character of the last phases of the third
fauna. From a comparison of the list of fossils supplied by Dr.
Schmidt with those of Bohemia, it appears that 21 species are com-
mon to both localities, of which 20 belong to stage E, and that, not-
withstanding the number of fish-remains, the highest zone of the
Isle of Oesel is anterior in age to stage G of Bohemia, but that fish
of many types appeared there at an earher period than than they did
in the Silurian basin of Prague.

In Sweden and Gothland stage E is represented by 22 and stage
F by 10 species common to those countries and Bohemia, thus con-
firming the views of Sir R. Murchison and Dr. Schmidt of the exist-
ence of the Wenlock and Ludlow rocks, the higher zones G and H
being entirely absent. In Norway, as in Sweden and Gothland,
nine-tenths of the species common to that locality and Bohemia
belong to stage H, stage F being but feebly represented ; beds referred
to the middle part of the Ludlow period being surmounted conformably
by unfossiliferous sandstones and marls 1000 feet in thickness, which
are considered by Prof. Roemer to be of Devonian age, In Thuringia,
Saxony, and Franconia, beds corresponding with the first phase of
Barrande’s third fauna, namely, zone E,. are succeeded by deposits
placed more or less high in the Devonian series. The Silurian rocks
of the Harz have been referred by Prof. Giebel to the horizon of the
Wenlock in England and zones E and F in Bohemia, and the presence
of Monoprion Sagittarius removes all doubt as to their Silurian age ;
but the mixture of Lower Devonian forms with those of the third
fauna, together with several types of fishes, and especially Ctena-
canthus, recall the upper calcareous zones F and G of Bohemia; but
the large number of species of Capulus which coexist with these fish-
remains in the Harz contrasts with the nearly total absence of that type
in zone G, whilst analogous forms are sufficiently common in zone F
and again in zone E; and although some Brachiopods, like Rhyncho-
nella cuneata, are referable to the former, the greater number apper-
tain rather to the latter. At present, therefore, the data are too
fragmentary and incomplete for the position of these beds to be deter-_

BARRANDE—-COLONIES. .§

mined with certainty (p. 211); but it is possible that further research
in the Harz may sooner or later confirm the facts observed in Bohe-
mia, of the sporadic appearance of fishes towards the close of the
Silurian period, along with Dalmanites, Bronteus, Acidaspis, and other
types characteristic of zone G (p. 212). Moreover, it is possible that
the deposits of the Harz form part of the great Paleozoic zone of the
north like those of the environs of Hof, and were separated from the
Bohemian basin by an ancient barrier of gneiss and other crystalline
rocks. In Spain, Sardinia, and France no beds higher than zone K have
been observed, unless it is in the department of the Lower Loire,
where M. Cailliaud has observed the coexistence of several’ species
characteristic of stage F, with others considered as Devonian.

Crossing the Atlantic, M. Barrande considers the North American
representatives of his third division of the Silurian system, and
arrives at somewhat different conclusions from those drawn by MM.
de Verneuil, D. Sharpe, and Hall. Excluding the Clinton and Medina
groups as passage-beds between the two great divisions of the system,
he includes the Niagara group and the whole of the Lower Helder-
berg series as representing his zone KE. Zone F is represented by the
Oriskany Sandstone, the remaining members of the upper Helderberg
series being regarded as representing generally zones G and H; and
he considers that, by means of certain Devonian forms in the Upper
Helderberg series, these beds are more intimately connected with the
Devonian system of Europe than are those of Bohemia, which contain
a smaller number of Devonian types.

Recapitulating his facts, M. Barrande observes that the countries
in the neighbourhood of Bohemia, namely, Saxony, Thuringia, and
Franconia, do not present a single trace of the last phase of the third
fauna, but that the first phase of this fauna is distinctly recognized.
The Silurian rocks of these countries appear to belong to the great
northern Paleozoic zone, like England, Russia, and the Harz, the
faunas of which present us with more marked connexions with the
phase of life appertaining to zones G and H.

Norway and Sweden, which belong to the same northern zone, and
are intimately related to England by the character of the earlier por-
tions of its Upper Silurian fauna, present none of the phases of
the latter part of that period. France, Spain, and Sardinia on the
contrary, although forming, like Bohemia, part of the great central
Paleozoic zone, and presenting the earlier phase of the third fauna,
are equally devoid of the latter portion ; but there are beds, considered
in France as representing the Lower Devonian system, which contain
fossils similar to forms disseminated through zones E, F, and G.

In England, the Isle of Oesel, and the Harz, zones G and H ap-
pear to be partially represented. In the Upper Ludlow and passage-
beds of England we find six genera of fishes associated with fossils
of Silurian types; but the Trilobites Dalmanites and Bronteus, and
the Cephalopods with a contracted orifice, characteristic of the higher
beds of Bohemia, are absent, as also are the Goniatites and Cardiola
retrostriata. In the Isle of Oesel, where the number of fishes
amounts to 43 species, among which are Coccosteus and Asterolepis,

6 * GEOLOGICAL MEMOIRS.

there are associated with them numerous fossils characteristic of |
the earlier period of the third fauna, whilst the Crustaceans and
Cephalopods appertaining to the latter part of that fauna are entirely
wanting. Inthe Harz, however, the presence of Ctenacanthus among
fishes and of Dalmanites and Bronteus among Trilobites, associated.
with forms of Devonian type, renders it probable that the limestones
of Magdesprung represent an epoch near those represented by stages
G and H (p. 266).

In the United States of America the closest analogy to the fauna
of Gand H is found in the Upper Helderberg group (especially in the
State of New York), which, by its Gasteropods, Acephala, and Bra-
chiopods, presents clearer connexions with the Devonian fauna of
Europe than do the similar zones of Bohemia.

With respect to the connexions between these two higher zones
and the Devonian system, after passing in review all the evidence to
be derived from organic remains, the author arrives at the conclusion
that generally they are not more directly united to the Devonian
fauna than are the higher zones of any of the other Silurian countries
where the third fauna has a less vertical development, and is even
reduced to its first phase; for if in Bohemia they contain the genus
Goniatites, which is not met with elsewhere, in the former they contain
several genera of fishes, and of other types, as Calceola, Grammysia,
Pleurodictyum, &e., which occupy a distinguished rank among Devo-
nian fossils, and which are completely wanting in the Bohemian
Silurian oe And, with reference to specific connexion, the two
upper stages in Bohemia contain fewer species identical with Devo-
nian forms, and fewer representative forms, than do the inferior
stages KE and F. In fact his researches lead him to the apparently
paradoxical conclusion that the two highest members of his third fauna
present less strong connexions with the Devonian system than do
those which immediately precede them.

Taken, therefore, from a paleontological point of view stages G
and H preserve completely a Silurian character, and are not united
to the Devonian system except by those usual links which announce
the approach of a succeeding period. [H. B. H.]

Erements of Cormicat and Puysicat Guotoey. By Dr. Gustav
Biscuor, For.Mem.G.S., &c. Vol. II. Second Kdition*.
[Lehrbuch der chemischen und pioeonlechen Geologie. Von Dr. Gustav
Bischof, For. Mem. G. S. Zweite ganzlich umgearbeitete ie Band IT.

Bonn, 1864.]

In this volume of the new edition of Dr. Bischof’s well-known
‘ Elementsof Chemical and Physical Geology,’ the whole of the material
of the former edition has been re-arranged, more especially with a view
to condensation, but, as alarge amount of additional matter has been
incorporated, the dimensions of the work are still very great, the

* Volume i. of this edition was noticedin Quart. Journ. Geol. Soc. vol. xx.
Part II. Miscel. p. 13.

BISCHOF——-CHEMICAL GEOLOGY. a

volume in question extending to not less than 952 pages of large
octavo size; the bulk would have been still further increased if all the
analyses contained in the first edition had been given in full, instead
of being merely referred to in foot-notes, as is done in several in-
stances. While in the first volume the general chemical principles
involved in the changes of the earth’s crust are set forth, the second
treats of the salts occurring in the mineral kingdom, taking the widest
sense of the term and according to the ordinary chemical classification.
The volume is divisible into three parts, the first comprising the Haloid
salts, the second the oxy-salts of acids which are easily soluble or
miscible in all proportions with water, and the third those of the
nearly insoluble silicic acid, or silicates. A fourth division treats of
the most important of the minerals which, in the author’s opinion,
have been produced from the decomposition of silicates. The volume
may in fact be regarded as a purely chemical mineralogy, in which,
without referring to their external characteristics, the composition,
formation, metamorphism, replacement, and decomposition of the non-
metallic minerals is considered, the metallic minerals being reserved
for a third volume.

The division into chapters is continued from the first volume,
commencing with chapter xvii. and ending with chapter xli. The
first chapter (xvii.) contains general remarks on the alkaline and
earthy chlorides, bromides, iodides, and fluorides, and on their presence
in crystalline rocks and lavas. Chapter xviii. is devoted to chloride
of sodium, under the headings of rock-salt and salt-lakes; the former
is shown to be deposited from sea-water by slow evaporation, on
account of its great purity, rock-salt being perhaps the nearest
approach to a pure chemical compound occurring in nature, some
varieties yielding by analysis 100 per cent. of chloride of sodium.
The salt from brine-springs, on the other hand, being produced by
rapid concentration of the solution, decrepitates when heated, portions
of the mother-liquor containing uncrystallizable chlorides being en-
tangled among the crystals. The great difference in the relative
proportion of gypsum and common salt existing in sea-water and in
saliferous rocks is explained by showing that, although sea-water
contains 16-4 times more salt than gypsum, the smaller absolute
amount of the latter salt represents 63 per cent. of the total necessary
for saturation, while the chloride of sodium only amounts to 7 per
cent. It is evident therefore that the solution will be sufficiently
concentrated to allow of the deposit of gypsum when 37 per cent. of
water has been evaporated, whereas it will be necessary to remove
not less than 93 per cent. before any salt can beseparated. In this
way the great masses of gypsum and anhydrite accompanying the
salt-masses of the Alps may be supposed to have been formed, by
partial concentration of sea-water which was removed before the salt
had time to be deposited. The notices of salt-lakes contain numerous
interesting particulars of the composition of the water of the Elton
Lake in the Crimea, which is remarkable for the large amount of chlo-
ride of magnesium, and the variable amount of common salt, that it
contains at different seasons of the year.

Chapter xix. treats of fluorides, the author noticing the combinations

8 GEOLOGICAL MEMOIRS.

of fluorine with other elements ; fluor spar, its production, association,
and pseudomorphic forms, and the more complex minerals cryolite,
topaz, and pycnite. It is suggested that the latter may be formed
from cryolite, a double fluoride of sodium and aluminium, when the
fluoride of sodium is replaced by a silicate of alumina, topaz being pro-
duced when the same replacement affects a portion of the fluoride of
aluminium.

In chapter xx. the alkaline and earthy carbonates are treated at
considerable length, commencing with the degree of solubility of
artificial and natural carbonates of lime; then follow the methods by
which calcareous pseudomorphs are formed. The carbonates of mag-
nesia, baryta, strontia, iron, and manganese are treated in a similar
manner, but the interesting subject of the formation of dolomite is
reserved for the next volume. The subject of the composition of the
‘natural carbonates of iron, sparry iron ore, clay-ironstone, black band,
&¢c., 18 most elaborately treated, no less than fifty-seven analyses of
these minerals being given.

Chapter xxi. treats of the different earthy sulphates, gypsum,
Epsomite, heavy spar, and celestine, their various methods of occur-
rence, transformations, &c. The difficulty of finding an origin for the
great masses of sulphate of baryta common in the newer mineral
deposits, no baryta-salt being recognizable in the composition of
crystalline rocks, is adverted to, as are also the recent researches of
Max Mitscherlich*, who announces the presenceof baryta, varying in
quantity from 0:45 to 2°33 per cent., in felspars from the Hifel and
S. Gothard. The production of sulphate of baryta by the double
decomposition of solutions containing witherite and gypsum is de-
scribed at length, with numerical illustrations.

Chapter xxii. on phosphates, commences with a notice of the various
minerals containing phosphoric acid other than the ores of the heavy
metals; the author then treats of Fownes’s investigations on the
presence of phosphates in crystalline rocks and lavas, and proceeds
to consider the solubility of the different substances containing phos-
phate of lime in water saturated with carbonic acid. This varies very
greatly, apatite requiring 393,000 parts of water for complete solu-
tion, while the scrapings of the bones of a freshly killed ox dissolve
in 4000 parts, and precipitated neutral phosphate of lime requires only
1500 parts. Phosphate of lime is formed when alkaline phosphates
are heated with silicate of lime. When phosphate of lime dissolved
in carbonated water is brought into contact with alkaline fluorides,
fluoride of calcium is deposited and phosphate of soda remains in
solution. This reaction is suggested as a probable cause of the increase
of fluorine in fossil bones. Phosphate of iron (Vivianite) is noticed
at some length, and a description is given of its occurrence in the
bones forming the skeleton of a drowned miner, which was found
in the Scharley zinc-mine in Silesia, upon reopening the workings
after they had been closed for three centuries. Vivianite may be
produced by double decomposition from apatite and sulphate or car-
bonate of iron. Notices of the best known occurrences of phosphates

* Pogg. Ann. vol. cxi. p. 351.

BISCHOF—CHEMICAL GEOLOGY. 9

n vegetable and animal structures, as well as in sedimentary rocks,

with remarks on the continued circulation of phosphoric acid from
the minerals, through plants to animals, and its return through the
decomposition of organic remains to the mineral state, close the
chapter.

Boracic acid and borates form the subject of chapter xxiil.; the
occurrence of boracic acid in the Suffioni of Tuscany associated with
sulphate of ammonia and chloride of ammonium is described ; and the
decomposition of boracite in the limestone from which the hot springs
rise is suggested as a means of origin. The formation of tourmaline,
&e., 1s reserved for the chapter on the origin of granite.

The third and most important part of the work, comprising chapters
xxiv. to xli., extending to nearly 600 pages, treats of the various sili-
cates found in nature, and the general remarks at the commencement
treat of their probable composition and origin. Of the former sub-
ject it is remarked that the formule in use for the more complex
silicates are of little other value than that of expressing the indivi-
dual views of the chemists by whom they are propounded. 'Through-
outthis portion of the work the composition of the minerals is expressed
chiefly by their oxygen quotients, that is the fractions obtained by
dividing the amount of oxygen in the protoxide and sesquioxide
bases taken together by that of the silica. With regard to the origin
of crystalline silicates, the author is disposed to consider them as
essentially formed by the action of water from amorphous masses ;
thus he remarks that, as a rule, lavas, especially those of newer date,
are not crystalline, although when sufficiently thick they may take
years in cooling ; this view is especially brought out in the conside-
ration of the origin of leucite, a mineral which occurs most abundantly
and in the largest crystals in Vesuvian lavas of pre-historic origin.
Even at ordinary temperatures glass becomes crystalline when ex-
posed to atmospheric changes for a long period, as has been shown by
Brewster and Zirkel in medieval glass taken from the windows of
Saint Andrew’s and Cologne Cathedrals.

The system of arrangement of the descriptive notices of the sili-
cates is based upon the relations of their pseudomorphs to each other,
the series being commenced with the zeolites, which never appear
except in their own proper forms ; felspar is made to take the second
place, from the fact that orthoclase has been found in the forms of
laumonite and analcime, and therefore may under certain circum-
stances be derivable from zeolites. The last members of the series
are the difficultly decomposable substances: mica, chlorite, steatite,
serpentine, &c., which are found as pseudomorphs of almost all the
harder silicates. Especial reference is made to the remarkable con-
trast between the extreme divisibility of mica due to physical structure
and its almost absolute stability against chemical changes from the
action of the air. This property is assumed to be due to peculiar
isomeric conditions of the component silicates. As might be supposed
in a substance forming the ultimate product of alteration of a great
number of different minerals, micas vary very much in composition,
the maxima and minima of the chief components are given as fol-
lows :—

yOL. XXIIJ.—LPART Il. C

10 : GEOLOGICAL MEMOIRS. _

SSW osnpaaa Gananehchaa: 36 per cent. min. 71 per cent. max.
JNIRDUOGUITE Sen penDe Soriaoc 6 55 38 ” »
Tron! Oxides \c.soneeeee 0 x 5 36 ” 9
Magnesia .........0. 0 99 92 29 9 9
Potash inis\siaeisVare\eietetaistale yy » ” 14 9 ”
POUT seme tance nee te Oars i» Oa ae 9
Fluor aieYeteusieleieialelottetevetetcle 0 19 ” 10-4 ” ”

Water is present up to about 4 per cent., and organic matter is
occasionally found in considerable quantity, as for instance in the
hithia-mica of Altenberg, which is treated in quantities of 16 cwts.
at a time for the production of lithia.

Serpentine forms the subject of chapter xxxix.; it is considered
throughout as a product of alteration, the view of its igneous origin
being distinctly repudiated. In like manner in the chapter on
quartz and other forms of silica the views of the so-called “ Plu-
tonists’”’ are combated to the uttermost. The volume is closed by
two chapters on magnetic and titanic iron-ores considered as pro-
ducts of the alteration of silicates, a view which is not generally
held in countries where those minerals are most abundant, as in
Scandinavia and North America. (B. By

On the Bracuiopons and other Bivatvezs of the Sr. Casstan Bens.
By Dr. Lave.
[ Proceed. Imp. Acad. Sciences, Vienna, March 23, 1865. |

Tur Brachiopods of St. Cassian offer a greater analogy in their
general facies with those of the Paleeozoic period than those of the
Mesozoic deposits, as Prof. Suess has already observed with respect
to the Brachiopod-fauna of the Hallstatt strata. At all events, the
St. Cassian strata represent an important period in the development of
this class, three Paleozoic genera, Cyrtina, Day., Spwigera, D’Orb.,
and Retzia, King, finding in them their last representatives; while
Spiriferina, D’Orb., not ascending above the Lias, first appears in
the St. Cassian strata. Among the other Brachiopods, Waldhemua
and Thecidium are Mesozoic; and Koninckina, Suess, and Amphi-
ceina, Laube, are peculiar to the strata in question, and are transi-
tion forms between the Palseozoic and the Mesozoic typical genera.
Among thirty species described, ten arenew. Only asmall number of
the fifty species described by Count Minster and Klipstein have
proved admissible, many of them being merely young forms of
established species. The Bivalve-fauna bears a more general cha-
racter, including however representatives of the typical Triassic
genera, Cassianella, Beyr., Myophoria, Bronn, and Hornesia, Laube.
This last genus, named after Dr. Hérnes, comprises the Gervillie of
the “‘ Muschelkalk,” bearing the type of G. socials, Schloth, and
differing from the genuine Gervillie by the peculiar structure of
their hinge, and by a more or less lengthened septum going through
the cavity of their umbones. Only about half the number of species
established by Count Miinster and Klipstein proved to be admissible
after. close examination, many of them having been established on
mere fragments, not offering any decisive characters, or on figures
of questionable accuracy. Of seventy Bivalves described by Dr. Laube,
only eight are new. [Count M.]

TRANSLATIONS AND NOTICES.
OF

GEOLOGICAL MEMOIRS.

On the piscoveRY iw Hartnavt, below the Sannvs referred by Dumont
to the THannr Sanps, of a coarse Limestone with a TERTIARY
Fauna. By MM. F.-L. Corner and A. Brrarr.

[ Note sur la découverte dans le Hainaut, en dessous des sables rapportés par
Dumont au Systéme Landénien, d’un calcaire grossier avec faune tertiaire ; par
MM. F.-L. Cornet et A. Briart. Bulletin de l’Académie royale de Belgique,
2me série, tome xx. no. 11].

Ar Tournay, Angres, and other localities in the southern part of

Hainaut, the Thanet Sands (Landénien inférieur of M. Dumont) are

seen overlying the Secondary formations, having at their base a glau-

conitic bed.which contains numerous badly preserved fossils. Among
these, however, there occurs abundantly an easily recognizable shell,
the Pholadomya Konincku of M. Nyst. MM.d’Archiac, Dumont, and

Hébert considered this bed to be the lowest of the Tertiary strata of

Belgium, and the equivalent of the “Glauconie inférieure” which

forms the base of the Tertiary formation of the Paris basin.

The object of the authors is to refute these opinions by proving
that there exists in Hainault, at a lower level than the glauconitic
beds of Tournay, &c., a fossiliferous bed, of which the described
species belong to a Tertiary stage of the Paris basin, superior to the
“Glauconie inférieure” of M. d’Archiac.

At Limbourg, in the environs of Heers, M. Dumont discovered
some marly and glauconitic beds lying below his <«‘ Landénien infé-
rieur ;”’ to these he assigned the name “ Heersien,” and classed
them with the Cretaceous formation of Belgium. M. Hébert, how-
ever, from paleontological and stratigraphical evidence, considered
them to be Tertiary, and Sir C. Lyell suggested the creation of anew
system, in which should be included the pisolitic limestone of France,
and the stages ‘‘ Heersien” and ‘‘ Landénien inférieur”’ of Belgium.

From this and other discoveries, the existence in Hainault of these
intermediate beds had long been suspected. At the beginning of this
year, M. Goffint sank a well on the confines of the town of Mons,
near the Obourg station, to the depth of 68 feet, when water was
reached. It presented the following section, in descending order :—

1. Grey sand, containing fragments of flint. 3 feet 6 inches to 4 feet.

2. An irregular bed composed of fragments of flint and phthanite. 4 inches
to 8 inches.

3. Yellow ferruginous sand, containing grains of glauconite. 8 inches to
12 inches.

4. Fragments of flint and of coaly phthanite. 4 inches to 6 inches.

5. Very glauconitic sand, very green, and a little argillaceous in the lower
part, but coloured and soft in the upper part; it contains fragments of phthanite.
15 feet 3 inches.

6. Very ferruginous red sand, containing limonite and numerous masses of a
VOL, XXII,.—PART IT, a

12 GEOLOGICAL MEMOIRS.

rock of the texture of sandstone, very slightly calcareous, of a red colour on the
outside, but a whitish grey in the fresh fractures: this rock contains numerous
fragments of indeterminable fossils; its present position seems to be the result
of areconstruction. 8 inches to 12 inches.

7. Yellowish or white limestone of a coarse texture; some of its bands are
compact, others very friable; in it occur certain beds, and detached fragments,
of a very hard white rock, 3 inch to 5 inches thick, entirely soluble in acids, and
some of them containing numerous cavities full of a pulverulent lignitic matter.

The appearance of some of the bands of the limestone reminds
one of the “ tuffeau”’ of Ciply and Maestricht ; but the difference in
their mineralogical texture is easily detected. The paleontological
evidence, however, leaves no doubt in this respect. An enormous
quantity of fossils, in a perfect state of preservation, has been pro-
cured from all the beds of the limestone, and even from the beds and
detached fragments of the harder included limestone. From 140 to
150 species have been collected, of which a great number appear to
be new. Of the known species, not one is Cretaceous; “all belong
to the Tertiary beds above the Glauconie inférieure of M. d’Archiac
and the Sables de Bracheux of the French geologists.”

The following is the list of the fossils which the authors haye
determined :—

GASTEROPODS.
Turritella intermedia, Desh.
imbricataria, Lam.
Voluta spinosa, Lam.
Ancillaria buccinoides, Lam.
Mitra terebellum, Lam.

Cerithium unisulcatum, Lam.

Melanopsis buccinoides, Fér.
Buccinum stromboides, Lam.

LAMELLIBRANCHS.
Cytherea multisulcata, Desh.
Cardita planicosta, Lam.
Crassatella compressa, Lam.
Corbula striata, Lam.
Corbis lamellosa, Lam.
Arca biangula, Lam.
modioliformis, Desh.
Tellina rostralis, Lam.

donacialis, Lam.
Lucina mitis, Sow.

Nerita Caronis, Brong.

Natica perforata, Lam.

epiglottina, Lam.
Monodonta Cerberi, Brong.

The greater number of the species which appear to be new be-
long to the genus Nematura, and some others to the genera Ancil-
laria and Auricula.

The authors then describe and compare several sections in the
neighbourhood of Mons, by which they endeavour to prove that the
glauconitic sand (no..5)-met with above the fossiliferous limestone
of the well of M. Goffint represents the base of the Landénien infé-
rieur, and corresponds to the beds of Angres and Tournay with
Pholadomya Koninckit.

Detailed sections at Ciply, Nimy, and other localities are given,
a complete section of which would represent the beds in the following
ascending order, resting upon an eroded surface of the chalk :—

Ist. A very glauconitic'sand, slightly argillaceous. In its lower
part the grains of glauconite are comparatively small and numerous,
and are imbedded in a matrix of a whitish-blue substance, which
gradually becomes softer towards the upper part, while the grains of
glauconite become larger and less numerous. To the south-west of
Mons it contains Pholadomya Koninckii, more or less abundantly,
and at Ciply a fossil of the genus Arca has been discovered.

}
i

j

5

CORNET AND BRIART—CALCAIRE GROSSIER OF MONS. 13

2nd.’Grey sand, slightly glauconitic, coloured yellow in some
places. Itis impossible to draw a sharp line of demarcation between
this and the lower bed, the passage of the one into the other being
characterized by an insensible diminution of the glauconite and the
white matrix, leaving nothing but a mixture of grains of quartz
with a few of glauconite, which gives to the rock a greenish-grey
appearance.

ord, Blue ferruginous clay, variegated with yellow.

4th. Very ferruginous yellow sand.

A section between Mons and Ath, obtained some years ago by
M. Lebreton-Dulier while sinking a shaft in a search for coal, is
described as affording evidence of the greatest importance. After
passing through 31 feet of black sand (surface-soil), and 26 feet of
grey sand containing some grains of glauconite, 20 feet of very green
sand was reached, repos'ng upon the débris of rocks, of which reliable
specimens were not obtained.

This green sand is in its mineralogical character identical with
that overlying the << calcaire grossier” of M. Goffint’s well (no. 5 of
section, p. 11); it rested upon a soft greyish-yellow limestone, con-
taining at different depths thin beds of hard white limestone. This
limestone was 305 feet thick, and contained fossils of which eight
species have been identified with those obtained from the well of
M. Goffint; they belong to the genera Nematura, Melanopsis, and
Cerithium.

The absence of Pholadomya Konincki from the glauconitic sand
to the north-east of Mons is ascribed by the authors to the softness
of the “white matrix” (see p. 12) in that district. This softness
decreases towards the south-west; and near Angres and Tournay,
in that direction, Pholadomya Koninckii is abundant.

The authors then trace the several beds which they have described
from the cemetery at Mons to about forty-four yards to the north of
the road to Charleroi, where they underlie the beds characteristic of
the “ Panisélien” system of M. Dumont, which are there seen in situ.
Upon this they remark that “‘ the glauconitic bed of our sections, and,
with greater reason, the limestone with the Tertiary fauna, which it
overlies to the north-west of Mons, are inferior to the ‘ Panisélien’
system and to the sandy and argillaceous beds which form the base
of it—beds which we refer, according to the geological map of
M. Dumont, to the ‘ Landénien’ and ‘ Yprésien’ systems.”

The “ calcaire grossier”’ of the well of M. Goffint seems to occupy
a vast depression or hollow in the chalk, and to correspond in its
paleeontological character to some parts of the upper sands of Sois-
sonnais (sables supérieurs du Soissonnais) and the “ Calcaire gros-
sier” of the Paris basin.

In conclusion, the authors point out other localities, in the neigh-
bourhood of Mons, where the same disposition of beds is known to
occur.

In reference to this subject M. d’Omalius d’Halloy, who, in con-
junction with M.Dewalque, reported on MM. Cornet and Briart’s
VOL. XXII.—PART IT. E

14 GEOLOGICAL MEMOIRS.

paper to the Academy of Sciences of Brussels, has comraunicated a
note to the Geological Society of France*, in which he discusses the
question whether the fossiliferous deposit discovered by them be not
comparable with the “Colonies” of M.Barrande. He concludes
that their discovery adds a new system to the Kocene deposits
hitherto known in Belgium, namely the “ Calcaire grossier of Mons,”
which underlies all the others, and which may be considered the
precursor of the Calcaire grossier of the Paris basin in a district
where that formation is not represented. He also remarks that the
existence of this small Eocene basin of “ Calcaire grossier of Mons,”
following the small basin of tufaceous chalk of Ciply, is a new indi-
cation in favour of the’ formation of calcareous deposits by causes
which are perpetuated or reproduced in the same localities. [A. 8.]

On the Environs or Toxay, Huneary. By Professor J. Szan0.
[ Proceed. Imp. Geol. Instit. Vienna, September 1865. ]

THE whole of these environs belong to the Tertiary period. The
eruptive rocks are trachyte and rhyolite; those of sedimentary origin
are the results of decomposed or disaggregated rhyolite; and last in
the series comes the soil producing the well-known wines. The
ascending order of the trachytes, as to their geological age, is :—
Andesitic trachyte (Baron Richthofen’s “ grey trachyte’’); amphi-
bolic trachyte (v. Hauer’s and Dr. Stache’s “genuine” or ‘red
trachyte’’), less extended than the first variety, but forming important —
and lofty mountain-groups in the south portion of the chain between
Eperies and Tokay; Beudant’s “Trachyte micacé amphibolique,”
the extreme link of the amphibolic trachyte near Vissegrad, is want-
ing in the Kegyallia or viniferous hill-range of Tokay. The rhyolites
differ from the trachytes proper by the crystallized quartz of primary
formation, and by the nature of the felspars entering into their com-
position, which contain a large proportion of silica combined with
lime and soda. Sanidine is but of subordinate occurrence. ‘The
rhyolites evidently owe their origin to submarine eruptions haying
taken place after the trachytes had been completely formed. The
two rocks, although once in mechanical contact, are in no way con-
nected as to their mode of formation. The marine shells included
in the rhyolites make it probable that their eruption began contem-
poraneously with the deposition of Leithakalk, and ended with the
beginning of the Cerithium-beds (consequently before the eruption
of the basalts of Northern Hungary, which are frequently in contact
with rhyolites and include fragments of them), while the trachytes
may be supposed to belong to the Oligocene or even the Eocene
period. The varieties of rhyolite are :—

a. Trachytic rhyolite, dark-coloured, porphyroid, passing into -
perlite, spherulite, and white tufaceous rhyolite. This is the type
of original rhyolite before its chemical and physical alteration by

* Bull. Soc. Géol. de France, 2™¢ série, vol. xxiii. pp. 11-13.

SZABO—TOKAY. 15

contact with sea-water, which, in the course of time, alters it into
vitreous clear-coloured varieties, then into pumice, and finally into a
white vitreous powder, which, mixed with larger fragments of these
and the preceding products of alteration, constitutes a pumice-con-
glomerate. _ The vitreous varieties give rise to obsidian- and perlite-
porphyries. :

b. Lithoid rhyolites, the substance of the upper portion of a rhyolitic
voleano, seem to have been produced by a later eruption, beginning
with vitreous substances, and pass’‘ng upwards into genuine lithoid
lavas. Dark. colours are of rare occurrence among them; the in-
cluded particles of quartz and felspar diminish to a very small size,
and sometimes the substance appears homogeneous. The lower por-
tions are homogeneous obsidian, the result of rapid solidification ; or
genuine perlite, sometimes with a nucleus of obsidian. Spheerulites
of radiated or dendritic structure are segregated from the rhyolites
of the Hagyallya.

c. Sedimentary breccias and tuffs, as mere agglomerations near
the places of eruption, and at some distance from them more or
less stratified with marine shells, as Cerithiwm ligmitarum, Arca, and
Pecten. These strata, solidified by infiltration, are Beudant’s “ mill-
stone porphyries.”” The younger tufaceous strata, subsequently
solidified by access of silica, lie nearly horizontally, and contain
species of Cerithiwm and Cardiwm of the Cerithian strata.

d. Rhyolitic trass, resting on the primary volcanic tuffs, efferves-
cing with acids, and partly decomposed into clay. The non-volatile
substances contained in the water of the sea, beneath whose level
these rhyolites have been raised, have had a chemical action on them.
In the first place, the oxide of iron has been converted into a soluble
substance, sesquichloride of iron, which, having been washed out,
left rocks of gradually paler tints, until the uppermost of them
became completely white. Then an addition of sodium may have
made them more fusible; and the sulphur of the pyrites which
was originally included in them, and of which traces still occur,
may have been oxidized into sulphuric acid, still occurring in the
white varieties of rhyolite (probably in the form of a mechanical
ageregation of sulphates and silicates). When submitted to red heat
and to decomposition under the action of water, these white rocks

treated with hot water give a considerable proportion of alum. An
extensive upheaval took place at the end of the rhyolitic period ; and
in consequence of it, several closed freshwater basins, excavated in
rhyolitic breccias and tuffs and receiving the waters of siliciferous
thermal springs, were formed around the margin of the group of
rhyolitic islands. The lowermost deposit in these basins is a stratum
of silicified mud, with specimens of Planorbis deprived of their calca-
reous shell. Then follows quartzite, with plenty of silicified trunks
of trees and other vegetable fragments, all transported by waters
from without,—or menilite, easily decomposed by water, the soluble
variety of silica occurring in the upper strata under the form of
white, loose, and very thin layers composed of Diatomacew, with
fine impressions of leaves on their planes of contact.

16 GEOLOGICAL MEMOILKs.

The productive soil around Tokay offers three distinct varieties :—
A. Argillaceous soil, immediately originating from the superficial
decomposition of trachyte, without any organic remains, not effer-
vescent with acids; this soil is the prevailing one, and gives the best
and strongest wines. 3B. Rhyolitic tufaceous soil, less fit for vini-
culture than A. C. Diluvial loam-soil, occurring to some extent
only on a hill next to Tokay, producing wines of inferior quality.

[Count M. ]

Eozoon wn Austria. By Professor HocustsrtEr.
[Proceed. Imp. Geol. Instit. Vienna, January 1866. ]

In South-western Bohemia an extensive system of strata, in which
metamorphic schistose rocks prevail, extends from the “ Bohmer-
‘wald’”’ and “ Bayrische Wald” to the north banks of the Danube.
This system, hitherto ranked among the Azoic rocks, is unconform-
ably overlain by the Ginetz beds, containing M. Barrande’s “ Pri-
mordial fauna,” and by Pribram Greywacke, in which Dr. Fritsch
has found traces of Annelids. Prof. Hochstetter, after long and
laborious search, succeeded in finding, in the crystalline limestone of
Krummau, agglomerations of calcareous spar and serpentine, which
have been declared by Dr. Carpenter, to whom specimens had
been sent for examination, to.be undoubted remains of Hozodn.
Prof. Hochstetter thinks the lenticular nodules partly composed
of calcareous spar and serpentine, so abundant in the vicinity of the
graphitic beds of Schwarzenbach and Mugerau, to be possibly of
organic origin. Prof. Giimbel, of Munich, has lately ascertained
the existence of Hozodn in the crystalline limestones of the “ Bay-
rische Wald.”

Prof. Hochstetter correlates as follows the pre-Silurian or Eozoic
strata of the “ Bohmerwald” and the frontier-mountains between
Bohemia and Bavaria, with the analogous formations in England
and North America :—

BouweEmia. ENGLAND. Nortu AMERICA.
a. Ginetz strata with M.

Barrande’s ‘ Primor- . Taconic system, or Pots-
dial fauna.” Spree [ dam Sandstone.
Pribram Greywacke.

6. Pribram slates ~ with
traces of Annelids.
Primordial argillaceous
slate.
c. Micaceous slate. ?
d. Prof. Giimbel’s “ Hercy- | Sir R. I. Murchison’s

Lower Cambrian

(Longmynd group). i Huronian system,

Upper Laurentian system.

nian” gneiss-forma- “ fundamental | Lower Laurentian system.
tion. gneiss” (partly).
e. Prof. Gimbel’s “ Bojic” Fist

gneiss-formation.,
[Count M.]

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

The Fauna of the Lowzr Oxutcocene Tertiary Beps of Hetmsranr,

near Brunswick. By Herr V. Kornen.

[Die Fauna der Unter-Oligocanen Tertiar schichten von Helmstadt bei Braun-
schweig. Von Herrn v. Koenen. Zeitschrift der Deutschen geologischen
Gesellschaft, Band xvii. pp. 459-534, 1865. ]

Tue author begins his Memoir with an historical notice of the dis-

overies respecting these middle Tertiaries from the time of Minster

and Goldfuss to the day when Beyrich introduced the term “ Oligo-
cene’”’ between the Eocene and. Miocene of Lyell, for beds, the
whole series of which only occur in North Germany, where they are
purely marine, and therefore can in that region only be fully
studied and understood. He then proceeds to point out what he
considers a want of due appreciation of the Oligocene system on the
part of Sir Charles Lyell, who places the Headon and Bembridge
beds in the Eocene, and the Lower Oligocene, on the other hand, in
the Miocene system. He calls attention to his Memoir published in
the Quarterly Journal for 1864, p. 98, in which he has shown that
the Headon series is the exact equivalent of the Lower Oligocene,
inasmuch as out of 56 marine species, 6 are peculiar to the Headon
series, and of the remaining 50, 43 occur in the Lower Oligocene,

23 being peculiar to it, whilst only 21 species occur in the Upper

Eocene (Barton). He then shows that every one of the 152 species

from Edeghem, as quoted by Nyst, occurs in the Black Sand (Lower

Crag) of Antwerp (‘Systéme Diestien’ of Dumont), and that con-

sequently it is incorrect to separate the Edeghem beds from the

Black Sand of Antwerp.

Herr vy. Koenen then points out the vast increase of material
which has been obtained for the better knowledge of the Oligocene
beds, since Prof. Beyrich first began his excellent work on the shells
of the North German Tertiary beds, but which he has so long left
incomplete. These fossils have been obtained chiefly from the
Middle Oligocene of Sollingen, and the Lower Oligocene in the neigh-
bourhood of Magdeburg. Other localities are also mentioned, most of |
which had been already alluded to by the author in a Memoir published
in the ‘ Zeits. d. Deutsch. Geol. Ges.’ 1863. p. 612, on the extent of
the fossiliferous beds of this formation. The green sands and yellow
clays of Helmstidt were then pronounced by the author to be Lower
Oligocene. Somewhat later Herr v. Strombeck, after a careful in-
vestigation of the beds in question, came to the same conclusion,
that they were Lower Oligocene. But in order to remove the possi-
bility of a doubt, Herr v. Koenen undertook the palzontological
question by carefully working out the fauna of the Helmstidt beds.
Numerous collections, both from German localities, and from Belgium
and England, were placed at his disposal, and he particularly alludes
to Mr. Edwards as having afforded him the greatest assistance.

The following section of the stratification at Helmstidt is taken
VOL, II.—PART II, E

18 GEOLOGICAL MEMOIRS.

from Herr v. Strombeck’s work, and is derived from a shaft sunk to
the brown coal about half a mile to the west of Helmstiadt.

ft. in
(a) Soil. R ee a at ead Neh 6 95
(G)iGraveley ei. eu oe aye!
(¢) Greensand ie a. ccs: We oc eee de en ee 30 8
(@Z) Greentclayswathvsand 5 \0ni a) n see .. 23.4
(¢) Grey calcareous sandstone .....-.)...7 4 2
(jf) (Green tmarhy ‘Sandiyn piel. coene see bls 4B
(g) Grey clayey sand with iron pyrites .... 10 10
(i) Brow coal). let et) anaes eee een 20 0

giving a total thickness of 95 feet 2 inches above the brown coal.
The fossils occur chiefly in bed f, except a few in e, but these are
identically the same as in f. The hard stone e is also petrogra-
phically the same as that which occurs sometimes in single blocks,
sometimes in tabular masses near Lattorf, Calbe, Eggersdorf, Neu-
Gottersleben, Aschersleben, Wolmirsleben, &c., with typical Lower
Oligocene fossils.

After describing the extent of the Brown Coal beds from Helm-_
stadt to Westeregeln, &., he refers to some grey-yellow clay beds
south of Helmstidt, which from their fossil contents, Cassis coronata,
Desh., Crassatella Woodui, v. Koenen, Pecten corneus, Sow.,.[socardia
multicostata, Nyst., Cardita latisulca, Nyst., Ostrea Quetelet, Nyst.,
and Ostrea ventilabrum, Goldf., must also be considered as Lower
Oligocene. The author then endeavours to correct the errors in the
nomenclature adopted by Prof. Giebel in his ‘ Fauna der Braunkohlen
Formation von Lattorf,’ owing to his want of proper means of com-
paring the Lattorf fossils with those of other localities ; and he adds
corrected lists of the fossils published on the four plates of Prof.
Giebel’s work, and warns geologists against the too hasty adoption of
Giebel’s names, and defends Mr. Edwards against the unfair charges
and attacks brought against him by Prof. Giebel.

Herr v. Koenen then proceeds to givea full and eritical description
of the 122 species (omitting five species of corals) which have been
found at Helmstadt, poimting out their analogues or identical forms
in other districts, and showing where the same species occur in other
Oligocene formations, or in older or younger beds; amongst these
are seven species of Cancellaria, 13 of Fusus, 4 of Oonus, 22 of
Pleurotoma, 5 of Voluta, 4 of Leda. This is followed by a tabular
statement of the whole Molluscous fauna of Helmstadt, from which
he deduces the following conclusions. ‘If we deduct from these
128 species the doubtful Nautilus imperiaks, Sow., and the 17 species
hitherto peculiar to Helmstadt, we have a remainder of 110 species,
of which 100 are known to occur in other Lower Oligocene localities,
whilst only 31 are known as Upper Eocene and 30 as Middle Eocene
fossils. There can therefore be no doubt that the beds of Helm-
stidt are also Lower Oligocene, the more so as, of these 100 species
59 occur only in the other Lower Oligocene, or in younger beds, but
not in older ones. The number of species which otherwise occur
only in the Middle Kocene, but not in the Upper Hocene, is only
four, namely Cancelluria subangulosa, Wood, var. rotundata,

HEBERT—-NUMMULITIC AND OLIGOCENE STRATA. We

v. Koenen, Pleurotoma turbida, Sol., var. ligata, Edw., P. attenuata,
Sow., and Solariwm pulchrum, Sow. He then alludes to the diffi-
culties occasioned by the anomalous occurrence of certain forms in
two distinct beds, when they are wanting in the intermediate bed ;
and he concludes with the hope that, although some modifications
may hereafter be rendered necessary, in consequence of. more perfect
materials for comparison, the labours of future explorers will be
facilitated by the work which he has already done, and the careful
comparison he has made. ! (NW Ee]

On the Nummounitic Strata of Norruurn Itaty and the Arps, and
on the Ox1cocENE of Germany. By M. E. Héserr.
, [Note sur le terrain nummulitique de I’Italie septentrionale et des Alpes, et
sur Voligocéne d’Allemagne ; par M. Hd. Hébert. Bull. Soc. Géol. de France.
Deuxiéme série. Tome xxiii. pp. 126-144. ]
‘The Tertiary deposits of the Northern Apennines dave been sub-
divided by the Marquis Pareto,* in the following manner :—

EocEne.

is tage Nicéen.—The Nummulitic limestones of Nice and the
Alps, overlain by great deposits of macignos and flysch.

2. Htage Ligurien.—Grey macignos, with alternations of lime-
Stones and argillaceous schists.

3. Htage Modénais or Calcaire a Fucoides.—The upper part of
the last stage where the limestones predominate.

MiI0cENnrE.

di Etage Bornmudien.—Beds of Dego, Carcare, &c., with Num-
mulites intermedia, with the intercalated lignites and lacus-
trine beds of the horizon of Cadibona. M. Pareto ultimately
classed in this division all the Nummulitic strata of the

, Vicentin and theVéronais, except Monte Bolca.

2. Hiage Langhien.—The marly grey sands, molasse, and ophi-
olitic sands of the Colline de Turin, characterized by fossils
,of the Faluns of Bordeaux.

3. Etage Serravallien.—Marly, grey, and yellow sands, &e.

M. Hébert considers it now possible, upon palaontological grounds
alone, to arrive at a more precise, and even a more detailed classifi-
cation that that of M. Pareto. In 1854, M. Renevier and the
author showed that it was necessary to detach from the great Num-
mulitic mass certain beds at Saint-Bonnet and Faudon, in the High
Alps, in the Diablerets in Switzerland, and at Pernant, Entre-
vernes, &c, in Savoy, which are overlain by the variegated sand-
stone and macignos to which the name of “ Flysch” has been given.
These beds, to which the term “ Terrain Nummulitique supérieur,”
was applied, are more recent than the other beds of the Nummulitic
series, and contain fossils characteristic of the Paris “ Calcaire gros-
sier”” and “Sables de Fontainebleau.” M. E. Sismonda adopted this
distinction, and in the following year discovered a still more recent
Nummulitic series in the valley of Bormida.

* Bull. Soc. Géol. France. Tome lxxi. p. 246.
E2

20 GEOLOGICAL MEMOIRS.

M. E. Sismonda referred all these groups to the Eocene, consider-
ing the middle one as the equivalent of the Eocene of the Paris
Basin. M. Pareto*, however, clearly showed a separation between
the Flysch and the “ Calcaires 4 Fucoides ” on the one part, and the
upper Nummulitic zone on the other; there is also an incontestable
relation between the true Miocene and this upper zone, which over-
lies, at Sassello and at Carcare, lignites with Cyrena Brongniarti,
Bast. (C. convexa, Brong.), and Cerithium margaritaceum, Broce.,
and which he considers the equivalent of the lignites of Cadibona.

From this it results that the great Nummulitic system of the
Alps and Northern Italy presents three groups of different ages,
namely, the Nummulitic formations (1) of Nice, (2) of the High Alps,
and (3) of Bormida, of which the two lower groups are Hocene, and
the upper one Miocene.

Two or three years ago the author procured a series of fossils from
the Vicentin, and while grouping them according to their localities,
was struck with the difference and the independence of the faunz so
separated. From an examination of these fossils he has concluded
that in the Vicentin there are different beds corresponding to the
different stages of the Tertiary series of Paris, namely :—

1. The beds of Priabona (Valle di Boro) are the equivalents of
the Biarritz, that is of the Lower, Kocene. To this level also belong,
on the one side Bolea, and on the other Brandola, and some. other
localities of Monte Berici, and probably also Val Rovina, and Monte-
glosso, near Bassano, to the north-east of Salcedo.

2. San Giovanni Ilarione and San Pietro Mussolino are synchro-
nous with the “ Calcaire Grossier Inferieur.”

3. Villagrande, near Ronca, is contemporaneous with the ‘‘calcaire
grossier supérieur,” including, perhaps, the “sables de Beauchamp.”

4, Castel Gomberto (Monte Grumi, San Valentino), Montecchio
maggiore (la Trinita), Monte Carloto near Monteviale, Monte Pos-
tale, and, further north, Salcedo to the north of Bregauze, and
Sangonini near Monte Sumano, and to the north-east Schio, cor-
respond exactly to the horizon of Gaas and the lower part of the
“‘ Sables de Fontainebleau.”

There is between Ronca and Castel-Gomberto a considerable gap,
which is filled up in the Alps by the hmestones with Nummulites
striata and NV. contorta, the Flysch, and the “ Calcaire a Fucoides.”
These deposits, then, become synchronous with the gypsum, and re-
present the Upper Eocene. The system of the valley of Bormida
presents a remarkable admixture of the fossils of the Lower Miocene
of Castel-Gomberto, and of the ‘‘ Sables de Fontainebleau” with the
middle Miocene fossils of Touraine and of the Superga. This system
is, then, posterior to that of Castel-Gomberto, and as it is anterior to
that of the Superga, it must be placed upon the level of the “ Cal-
caire de Beauce,” of which it constitutes the marine equivalent.

The author then gives it as his opinion that the mountain masses
to the north, in the Vicentin and the Véronais, and to the south, in
the Ligurian Apennines, which form the great basin of the Po, have
been during the Tertiary period subjected to an oscillatory move-
ment, which aliernately elevated the northern and depressed the

* Bull. Soc. Géol. France, 2¢ Sér., tome xii. p. 370.

HEBERT—NUMMULITIC AND OLIGOCENE STRATA. 21

southern part, and vice versd, during which the deposition of the
several beds was taking place.

In the long succession of faune and physical phenomena de-
scribed by M. Hébert, it is between the Nummulitic fauna of the
High Alps and that of Castel-Gomberto that the greatest difference
is manifested, and it is there where M. Pareto, incorrectly as the
author thinks, places the limit between the Miocene and the Eocene.

An intimate relation exists between the beds of Castel-Gomberto
and Salcedo, and the Upper Nummulitic beds of the Bormida, and
between these latter and the true Miocene of the Superga, and of
Léognan, or of Touraine.

An altogether analogous succession unites together, in Aquitaine,
Gaas and Léognan, and M. Hébert considers that at present it does
not appear necessary to add to the three great divisions of the Tertiary
a fourth—the Oligocene,—which is included in his Lower Miocene.

If in the north of Europe this Oligocene presents great differences
from the Miocene (Middle Miocene), it only shows that the upper
part of this group is not generally represented by a freshwater forma-
tion; but the continuity is found again in the south, and there it is
not possible to admit the Oligocene. There is not then sufficient rea-
son to change the ternary division of the Tertiary strata, and the
best line of demarcation between the middle and lower group will
‘remain that which, in a general manner, M. Elie de Beaumont has
indicated, namely, below the F ontainebleau sands, and which the
author has attempted to define more clearly by fixing it between
the freshwater marls above the gypsum, and the marls with Cyrena
convexa and Cerithium plicatum, &c., below the Calcaire de Brie.

A paper by M. Beyrich, published in 1858, in the “ Berichte” of
the Academy of Berlin*, is then noticed by M. Hébert, who says
that the author has, in some instances, given to his statements a
meaning which was not exactly intended. For instance, his opinion
that although the sea of the Faluns of Touraine differed as much
from the sea of the Fontainebleau sands, as these from the sea of the
*‘ Calcaire grossier,” it was preferable to adhere to the ternary divi-
sion, has been rendered altogether differently in the German text.

M. Beyrich has placed the Fontainebleau sands as the equivalent
of his Middle Oligocene, and the gypsum of Montmartre as syn-
chronous with the Lower Oligocene, which would be represented in
Belgium by the lower beds of Limbourg. This classification, M.
Hébert thinks, cannot be justified by facts. First of all, in the
Paris basin the gypsum belongs certainly to the lower part :—

(1) By the marine bands intercalated with its lower beds, of
which the fauna is identical with that from the marls with, Phola-
domya Ludensis, which belong to the Beauchamp sands; (2) by
the freshwater beds above the gypsum, the fauna of which ap-
proaches nearer to that of the Saint-Ouen limestone, situated below
the gypsum, and the marine marls with P. Zudensis, than of that
of the Brie limestone; (8) by the contained Mammifers, which it
would be difficult to associate with those from the Beauce lime-
stone, this being the consequence of classing the latter as Upper
Oligocene, and the gypsum as Lower Oligocene.

* See also Quart. Journ. Geol. Soc. vol. xx. Part 2, Miscell. p. 5.

-

22 GEOLOGICAL MEMOIRS,

In the second place, the fauna of the Lower Oligocene, as far
as the author was able to judge in his journey to Latdorf, seemed
to be singularly analogous to the fauna, not of the first marine
beds of the Fontainebleau sands, but to those of Morigny, near
Etampes, superior to the marine marls of Montmartre. From
Latdorf about torty species were obtained, and the author has not
been able to establish the identity of one of them with Eocene
forms. While admitting that the fauna of the Lower Oligocene
may be anterior to that of Morigny, he considers that there is still
enough margin between this zone and the gypsum in which to
class it, without separating it from the Lower Miocene; for in the
Paris basin, between the horizon of Morigny and the freshwater
marls above the gypsum, which M. Hébert considers as the upper
limit of the Eocene, there are, (1) sands and marls with Natica
crassatina, Deshayesia cochlearea, Brong., &c. (2) Freshwater lime-
stones and ‘“‘ meulicres” of Brie. (3) Green and yellow marls with
Cyrena convexa, Brong. sp., Psammobia plana, Brong. sp., Ceri-
thium plicatum, Lam., C. trochleare, Lam., Bithynia plicata, d’ Arch.
and de Verneuil, sp.

There is not sufficient reason to place the Lower Oligocene below
the last of these.

The lignites upon which the marine beds of Latdorf rest, and
generally the Lower Oligocene, may, the author admits, possibly cor-—
respond to the gypsum, although it is impossible to assign a definite
place to it until after the discovery in it of organic remains. He
also thinks that the beds of Limbourg may be ranged with the
Middle and Lower Oligocene of M. Beyrich, but considers that too
much haste has been shown in identifying the Lower Oligocene of
Belgium and Germany with the Upper Eocene of England, especi-
ally with the Barton clay.

The idea of a general catastrophe putting an end to the Eocene
fauna, which had been attributed to the author by M. Beyrich, is
denied, and a more gradual operation, such as accompanies all general
movements of the surface, is maintained to have been the cause.
The author then gives a Table showing the correlation of the beds
belonging to the Lower Miocene in France, Germany, and Beigium.

France. Germany. Belgium.
(
3 | Upper bed ...|Beauce limestone. [Upper Oligocene . ;
3 § | Middle bed.../Sands of Etampes .|Middle Oligocene .|Upper Limbourg.
Bod
4 = j Brie limestone and
Lower bed marls with Cy-| } Lower Oligocene|Lower Limbourg.
ROME! peisit lb das
? Lieni = te
Upper Eocene ...... Gypsum ...... { ; i Oa | Missing.
see Gece eal Beauchamp sands |Missing ............ Missing.

per bed)

_ M. Hébert attempts to show that it 1s more probable that the
Middle Oligocene of the basin of the Rhine, and of Switzerland is
related to the beds of Tongres and of Maestricht than, as M. Bey-

GUMBEL—EOZOON IN BAVARIA. : a3

rich considers, to those in the environs of Orléans, and he denies
that he, in conjunction with M. Renevier, ever asserted that the
Nummulitic strata of the High Alps are contemporaneous with the
«Sables de Fontainebleau ;” but, on the contrary, that he had
refererd them to the gypsum. |

Lastly, M. Hébert says he is still of opinion that the Barton clay
is synchronous with the lower part of the Beauchamp sands, and the
Headon sands with the upper part. The upper part of the beds of
Colwell Bay belong to the Fontainebleau sands, and the fossils of the
gypsum are found between these two horizons in the freshwater
formation of Hordwell. No newreason has been shown for classing
the gypsum in the Lower Oligocene.

The conclusions at which the author has arrived are these :—that
the Lower and Middle Tertiary series, regarded in the north and
south of Europe, present their maximum of difference, both palzon-
tological and stratigraphical, between the gypsum and the base of
the Fontainebleau sands on the one part, and between the Flysch and
the beds ef Castel-Gomberto on the other ; and that it is there where
the limit between the Eocene and the Lower Miocene, or Oligocene,
should be placed. This last is allied much more with the Miocene,
properly so called, or Middle Miocene, than with the most recent
Kocene beds.

At the epoch of the gypsum the sea retired from the north,
where, in the opinion of the author, there does not exist any marine
equivalent of the beds with Palcotheriwm, and advanced to the
south, where it penetrated to the Alps, and occupied a part of
Switzerland, but without communicating with the depression already
existing in the valley of the Rhine. Afterwards, when at the com-
mencement of the Miocene epoch, the sea extended to the north of
Germany, it withdrew from the Alps to the Vicentin gulf. On both
sides, it seems well proved that during the period which this study
embraces, it was at this time that occurred the greatest differences
in the general distribution of sea and land in Europe. [A. 8.]

On the OccunRENCE of Kozoon in the Primary Rocks of Eastern
. Bavaria. By Prof. Gumset,

[Ueber das Vorkommen von EHozoon in dem ostbayerischen Urgebirge. Von
Herrn Giimbel. Sitzungsberichte der konigl. bayer Akademie der Wis-
senschaften zu Miinchen. 1866, I. Heft 1. pp. 25-70. 3 plates.]

Prof. Gimbel introduces the special subject of his memoir by a
concise exposition of the facts relating to the discovery and deter-
mination of Hozoon, including its structure, mineral condition, and
geological position. He then describes the geological features and
relations of the older rocks of Bavaria, which he arranges in descend-.
ing order as follows :—

1. Hercynian clay-slate.
2. Hercynian mica-schist.
3. Hercynian gneiss.

4. Bojic gneiss.

The Hercynian gneiss is considered to be equivalent to that of the
Danube, and both are stated to abound in layers of graphite, which

24 GEOLOGICAL MEMOIRS.

the author thinks is important as proving the existence of organic
life at the time of their deposition. The Hercynian and Bojic gneiss-
formations together are held to represent the Lower Laurentian
system of Canada; the Hercynian mica-schist, the Upper Lauren-
tian or Labrador series ; and the Hercynian clay-slate, the Huronian
of Canada and the Cambrian of England. Prof. Giimbel then de-
scribes the mineralogical characters of the Hercynian gneiss, and
afterwards shows that a stratified ophicalcite occurring near Stein-
hag, exhibits structures corresponding with those of the Canadian
Hozoon in addition to other appearances which he also believes to be
of organic origin, and some of which he compares to the sections of
certain Bryozoa.

The occurrence of a second species of Hozoon, to which he gives
the name Hozoon Bavaricum, has been discovered by him in a rock
consisting of a granular aggregation of calcite, serpentine, and a
white hornblendic mineral, arranged in flakes or stripes. The rock
belongs to the Hercynian Clay-slate formation, supposed to be of
Huronian or Cambrian age, and the specimens examined were ob-
tained from near Wunseidel and Thiersheim, and between Hohenberg
and the Steinberg, especially the last-named locality. It exhibits:—
(1) A thin band aimost entirely calcareous, and traversed by a network
of straight lines, or, when treated with acid, divided by band-like ribs
into irregular cell-like spaces, the calcite filling which is seen to be
granular. (2) Thicker calcareous portions abounding in tufts of fine
tubes, exactly as in Hozoon; these tubes end at the serpentinous
portions (3), which have generally the same form as in the Hozoon
from Steinhag before described, but are much smaller. In decal-
cified examples they may be seen to possess the same vaulted mar-
gins as Hozoon; their breadth averages -1 millim. and the diameter
of the tubes ‘01 millim. Generally these serpentine bands pass into
an adjoining portion (4), of one-half the width, or less, made up of
very much twisted lamelle, consisting of serpentine or a whitish mi-
neral, and possessing highly vaulted and deeply channelled outlines.
Prof. Gimbel considers that on the whole these characters un-
doubtedly prove the affinity of this more recent and very much smaller
form to the group Hozoon; but as the last-mentioned structure (4)
differs from what has been observed in Kozoon Canadense, he gives
it the distinctive name of Hozoon Bavaricum*.

In conelusion Prof. Giimbel describes certain structures which
appear to indicate with greater or less probability the presence of
Eozoon in the pargasite of Pargas in Finland, in the coceolite-lime-
stone of New York, in ophicalcite from Tunaberg, in a granular lime-
stone containing chondrodite, hornblende, and garnet, from Boden
in Saxony, in a blackish serpentinous limestone from Hodrisch in
Hungary, and in ophicalcite from Reichenbach in Silesia.

(H. M.J.]

* Dr. Carpenter has lately recognized the similarity of the Connemara
Eozoonal structures to those of Hozoon Bavaricum (supra, Part 1, p. 228). This
observation is of considerable interest when viewed in connection with the rela-
tive geological age of certain Eozoonal rocks, more especially the probable Cam-
brian date of Hozoon Bavaricum, the Lower Silurian position of the Connemara
serpentine, and the Laurentian age of Hozoon Canadense,—Epit.

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Exriorations made during the WintER of 1865-66 in the
Caverns of the banks of the Lussr. By M. E. Dupont.

[Etude sur les fouilles scientifiques exécutées pendant Vhiver de 1865-66
dans les cavernes des bords de la Lesse, par M. E. Dupont. Bull. de l’ Acad.
Royale de Belgique, 2me série, tome xxii. ]

Caverns of Pont a Lesse.—Several little caverns occur in the com-
mune of Anseremme, about a quarter of a mile down the river, from
the castle of Pont 4 Lesse. They are upon the right bank of the
river, and about 30 to-40 feet above its level. One of the principal
of them presented the following section in descending order:— __-

1. Greyish-yellow earth, 2$ feet.

2. Dust, 9 inches.

3. Black earth containing human bones, bones of animals, numerous land
shells, with abundant fragments of pottery, some pieces of flint, ashes, &c.,
12 foot.

“4, Yellow clay, 2 inches.

5. Grey earth, sometimes encrusted with stalagmite. Human bones, bones
of animals, as in bed No. 3, flint, numerous fragments of pottery, ashes, and
coals, and plates of psammite. 2% feet.

_ 6. Yellow clay, 5 feet.
7. Traces of yellowish-white pure sand.

The yellow clay with angular fragments of limestone (No. 6),
which is only separated from No. 7 by traces of sand, is easily recog-
nized as the equivalent of the argillaceous deposit which overlies
the whole province, being the ordinary yellow clay with blocks
(argule jaune a blocaux) forming the base of the upper stage of the
Quaternary formation of this region, and containing in other cases
the remains of man, and of a fauna of the age of the Reindeer. The
superposed beds are consequently posterior to that age. The occur-
rence in them of a very coarse pottery indicates a pre-Roman
date, a determination which is confirmed by the presence of frag-
ments of flints and of two worked flints, together- with a little
flint arrow-head “ @ ailerons,” so characteristic of the age of polished
stone.

Remains of this age are found at two levels. The first is only
separated from the “ argile a blocaux” by masses of limestone coming
from the partition of the cavern. It furnished fragments of grey
pottery with grains of unburat calcareous spar, not modelled with
the hand, some plates of baked flint, two worked flints, a flint
arrow-head, a fragment of the tusk of a wild boar pierced with a
hole, ashes, and coal, some burnt bones, plates of psammite, and
some rolled flints. It also contained human bones, together with
bones of the Wild Boar, Goat, Stag, Heath-cock, Water-rat, and

VOL, XXII.—PART II. F

26 GEOLOGICAL MEMUIRS,

three vertebrae of a large fish (? Pike). Helix nemoralis, Helix
lapicida, and Unio batavus were also found associated with them.
The author remarks that the occurrence of human bones in the
midst of the remains of the repasts of men is at present inexplicable,
and rejects the hypothesis that it may indicate cannibalism on the
part of the inhabitants of the cave.

In the beds overlying the “argile 4 blocaux,” which, M. Dupont
considers, occupies the place of the loess, an almost complete human
skeleton of enormous dimensions was found; the contour of the
grave in which it had been buried could be distinctly traced: and
afterwards five other skeletons were found in a common grave.
Neither arms nor any other object by which their age could be de-
termined were discovered; and, excepting that they are posterior
to the age of polished stone (for the graves are dug in the deposit
which overlies remains of this age), no period can be assigned to
them.

Between Chaleux and the castle of Walsin occur several caverns,
three of which the author describes.

Trou des Blaireaux (Tré des Tassons).—After passing through a
yellow earth almost without blocks, an unstratified yellow clay with
blocks is reached. Besides some ashes and a rudely cut block of
baked flint, bones of the following species were found :—Horse, Elk,
Fox, Otter, Badger, Wild Cat, and Heath-cock, the bones of the
Badger being particularly numerous. Below this was a bed of alter-
nating veins of clay and sand, with two beds of gravel. This sandy
argillaceous deposit is certainly the ‘‘ Lehm.”

Trou de v Hyéne.—This cavern is nearly opposite the “ trou des
blaireaux,” upon the opposite bank of the Lesse; it has two open-
ings, is about 12 feet above the river, and presents the following
section :—
is hs a ah formed by dead leaves, and containing bones of the Fox and

Owl.

2. Yellow clay, containing bones of the Reindeer and the Horse, as well as two
worked flints. j

3. Thin and non-continuous bed of stalagmite.

4. A sandy argillaceous deposit of a greyish-yellow colour, with traces of stra-
tification and rolled pebbles.

Numerous bones are found in this bed, belonging principally to
the following species :—Hycena spelea, Great Bear, Fox, Horse, He-
phas primgenius (milk tooth), Rhinoceros tichorhinus, Ox (two spe-
cies ?), and Reindeer.

The most abundant remains belong to the Hyzna, Rhinoceros,
Reindeer, and the Horse; and nearly all show traces of a strong
carnivore, except the Hycana, from which it may be inferred that
this cavern was the den of that animal, the other bones being the débris
of itsrepasts. ‘The results attained by the exploration of this cavern
are of the highest importance ; for by them we are enabled to assign
the place of the great Quaternary mammifers to the stratified sandy
argillaceous beds or Lehm, they evidently haying lived immediately
before the deposition of these strata. On the one side the stratified

DUPONI—CAVERNS OF THE LESSE, 27

sandy argillaceous beds occur, as well in the caverns as in the sub-
aérial formation of the province of Namur, between the great deposit
of rolled pebbles on the one hand and the argillaceous deposit with
blocks on the other.

But, as in the valley the deposit of rolled pebbles is characterized
by the abundant remains of Elephas primigenius, these beds may be
named the beds with Elephas primigenius (couches & Elephas prim-
genius). On the other side, the deposit of yellow clay with blocks,
which is the equivalent of the diluvium rouge of the Paris basin,
contains the fauna of the Reindeer properly so called, the charac-
teristic of which is the absence of extinct species, and the presence of
a series of animals which are at present banished to colder climates.
These facts confirm, in the author’s opinion, his division of the Qua-
ternary formation into three stages :—

Etage superieur a Cervus tarandus.
Ktage moyen a Ursus speleus.
Etage inférieur 4 Elephas primigenius.

Trou de la Naulette—This cavern is on the left bank of the Lesse,
about 60 yards up the river from the “ trou des blaireaux.” It is
27 feet above the river, is more than 40 yards long, and has a
breadth in the middle of 12 yards. At the entrance to the cavern
was a thick deposit of yellow clay with blocks, containing bones of
the Horse, Reindeer, &c., which thinned out so rapidly that at
4 yards from the entrance there was not more than a trace of it.
There a falling in of part of the roof had completely hidden the
Quaternary deposits. ‘Towards the extremity of the cavern, some
well-stratified sandy argillaceous beds were laid bare, not overlain by
the clay with blocks. A sinking made here presented the following
section :—After passing through 9 feet of sandy clay and yellow sand,
followed by 14 inches of yellow clay with fallen stones (a), cones of
stalagmite, and bones of ruminants, 4} feet of alternating beds of
clay and stalagmite were reached. ‘This was followed by sandy clay
and sand, about 4 feet in thickness, which contained at its base the
head of a Wolf and some vertebrae. In this bed (6) nearly all the
bones mentioned hereafter were found. Below this, beds of sandy
clay and sand were reached, followed by a gravelly sand, until traces
of red clay were discovered.

The bone-bearing beds occurred at two levels. The upper one (a)
contained some bones (especially single rami of the jaw) of an unde-
termined Ruminant.

The lower level (6) furnished, however, the most important series
yet obtained from the caverns on the banks of the Lesse. The bones
were not numerous, but were in an admirable state of preservation.
The principal species were the Wolf, Ursus arctos, Fox, Badger,
Bat, Marmot, Water-rat, Elephas primigenius, Rhinoceros, Horse,
Reindeer, Wild Boar, Chamois, Common Stag, Sheep, and a fish.
But the great importance of the discovery consisted in the presence
in the midst of the bones of a human jaw and cubitus, and of a bone
with a hole artificially produced. The association of the human
remains with the rest of the bones was beyond a doubt.

28 GEOLOGICAL MEMOIRS.

The author then gives a detailed description of the human jaw
and cubitus, and compares the former with the one discovered asso-
ciated with remains of Hlephas primigenius and Rhinoceros ticho-
rhinus in the grotto of Arcy by M. de Vibraye, and with a jaw of the
age of the Reindeer which came from the “ trou de Frontal,” with both -
of which, notwithstanding that the latter is of a much more recent
geological age, he declares it to have a most intimate connexion.

Several bones, associated with these human remains, seemed to
bear traces of the hand of man, especially a fragment of a bone which
may be referred to a ruminant. The hole which is pierced is evi-
dently artificial, the sides of the incision being very sharply cut.
The sides of the fragment appear cut with a sharp instrument,
unless, as M, de Quatrefages suggests, it be a particular mode of
fracture, (Ais Red

. >

On THREE CAveRNS in the VautEy of the Lussn EXPLORED during the
months of Marcu and Aprit 1866. By M. EK. Dupont.

[Etude sur trois cavernes de la Lesse explorées pendant les mois de Mars et
d’Avril, 1866, par M. Edouard Dupont. Bull. de PAcad. Royale de Belgique,
Qme sér. tome xxii. ]

Trou de Praule.—The cavern of Praule is situated on the left bank
of the Lesse, about 600 yards up the river from Furfooz. It is easy
of access, and about 98 feet above the level of the river. The cave
is 194 feet broad, and has a length of 11 feet in the centre, its mean
height between the rocky floor and the roof being little more than
63 feet.

“Upon the calcareous soil is a thin bed of sandy stratified clay,
with rolled pebbles and gravel in non-continuous veins—the cha-
racteristic of the Lehm, or middle stage, of the Quaternary formation
of Namur. The deposit yielded a humerus and a canine of a Great
Bear, which, the author , considers, confirm the application to this
Lehm of his name of “ Htage a Ursus speleus.”’ These beds are over-
lain by yellow clays with blocks (argiles jaunes 4 blocaux), which
contain, especially at the base, worked flints and bones of the Bear,
Wolf, Fox, Horse, Reindeer, and Goat. ‘The flints worked in the
form of a knife are few, and are derived from the Chalk. The bones
are probably the remains of repasts of men, as is generally the case
in deposits of this nature in the caverns of the banks of the Lesse.
These facts prove, in the author’s opinion, that the argile a blocaux
should be referred to the age of the Reindeer, and is relatively
anterior to the deposition of the vast covering of clay. To the beds
thus characterized, which form the upper stage of the Quaternary
formation of the province, M. Dupont gives the name of “ Ftage a
Cervus tarandus.”

Trou des Allemands.—The shelter furnished by a sloping dolo-
mitic rock, under which the Bohemians established themselves
during their wanderings, constitutes this cavern. Shelters of this
kind are very numerous along the banks of the Lesse, and are
generally slightly raised above the river-leyel. The following is the

DUPONT—CAVERNS OF THE LESSE. 29

section presented by one near the route from Hulsonniaux to Celles,
in ascending order :— .
5, Rolled pebbles of Ardennaise origin cemented by gravel.

4, Yellow clay with dolomitic blocks.
3. Loess.

2. Alluyium formed of alternating veins of sands and clays, like Lehm.

1. Like No. 2, but vemaniés and mixed with vegetable detritus. From this
bed the author obtained some flint knives and a little sandstone hache, polished
and with an irregular surface.

Nutons des Gendron.—The cavern of Nutons desGendron is situated
on the right bank of the Lesse, about 14 mile (in a direct line) from
the Furfooz cavern. It is excavated in a schistose bed with alter-
nating calcareous bands, belonging to the “‘ Psammites of Condroz.”
The length of the cave is 15 yards, and it has a breadth at the
opening of 23 yards. At the entrance is a mould formed by the
decomposition of leaves, below which is found yellow clay with
blocks of schist, without bones or works of art. The mould ata
distance of 8 yards from the entrance was overlain with stalagmite,
and contained human bones which belonged to no less than seventeen
skeletons. Although the bones were broken, the workmen were
able to observe that fifteen of the skeletons were arranged longi-
tudinally along the cavern in six rows of two or three, varying
according to the width of the cavern, with two skeletons placed
transversely, the heads of the longitudinal skeletons being towards
the mouth of the cave. A very small splinter of chalk-flint in the
shape of a plate was found, together with three fragments of coarse
pottery.

On the slope of the escarpment, immediately below the entrance,
two great blocks of transported schist were dug up, one measuring
5 feet by 2? feet, the other 34 feet by one foot.

Among the human remains were found bones of the Fox, Badger,
Fowl, &c. The workmen also found a modern metal button with
inscription, but without a date.

After having noticed the great number of human bones, especially
fragments of the upper and lower jaw, and given detailed descriptions
of the bones, the author states as his opinion that the remains are
in a sepulchral cavern. The exact age, however, to which they
belong is difficult to determine. The skeletons belong to a period
posterior to the age of the Reindeer, because in the province of
Namur remains of that age are always found below the yellow clay,
the mould in this instance being above. M. Dupont therefore
concludes that the skeletons were deposited in the cavern at an
epoch posterior to the age of the Reindeer and anterior to the
Bronze age, and refers them to the Polished-Stone period (dge de la
pierre polie). [A.8.]

On a New cunvs of Cupnatorvops. By Chev. F. von Haver.
[Proceed. Imp. Acad. of Vienna, December 14, 1865. ]
Tuis genus, for which the author proposes the name of “ Ohoristo-
ceras,” bears a shell similar in form to that of Orioceras, with the

30 GEOLOGICAL MEMOIRS.

lobular ornamentation characteristic of Ceratites. The first speci-
mens of Choristoceras Marshi were brought to Vienna by Mr. O. C.
Marsh, F.G.8., of Newhaven; subsequently Prof. Suess received a
greater number of them; and lately Mr. Hinterhuber, an Imperial
Mining Engineer entrusted by the Imperial Geological Institute
with the task of examining the locality of the specimens found in
Austria, ascertained their occurrence in a stratum resting on un-
doubted Kossen strata and overlain by “ Adneth” (Liassic) lime-
stones. Similar forms occur among the specimens referred to “ Crio-
ceras,”’ from the Bavarian Alps, described by MM. Giimbel and Schaf-
hautl; but their determination must remain uncertain until their
lobular ornamentation becomes better known. [Counr M.]

On Remains of the Marmot (Arctomys marmota, G'mel.) im STYRIA.
[Proceed. Imp. Acad. Vienna, 8th and 22nd March, 1866.

Tur remains of this animal, which has never been known in Styria,
as far as historical records or traditions go, consist of a jaw, found
at the junction of the Parschlug and Mirz valleys, among some inde-
terminable fragments of bones; it was recognized as belonging to
the species in question by Prof. Hyrtl (sce Imp. Geol. Instit., Annals,
xiv. 1864, Proceedings, p. 33). In the beginning of 1866, Prof.
Oscar Schmidt discovered again, in the neighbourhood of Gratz,
about two hundred feet above the river Miirz, an old den of Mar-
mots, with the skeletons of four individuals, belonging to three
different generations. These animals must be supposed to have
lived in Styria during a portion of the Diluvial period, when the
extension of glaciers in the higher Alpine regions drove away the
Alpine flora and fauna to seek shelter and food in lower, and con-
sequently more congenial, regions. [Count M.]

rr

The Gastmrorons of Sr. Cassran, By Dr. Lavss.
[ Proceed. Imp. Acad. Vienna, May 11, 1865.]

Tur Gasteropod-fauna of St. Cassian possesses many species analogous
to forms found in the Carboniferous Limestone, and is particularly
interesting as being a “ Limit-fauna,’”’ comprehending representatives
of a number of undoubtedly Paleozoic genera associated with others
whose full development took place afterwards in the course of the
Mesozoic Period; and the number of species occurring also in other
localities is but small. The types of two new genera have lately been
discovered among the Pectinibranchiate Gasteropods of St. Cassian,
namely (1) Huchrysalis, having a chrysalid-like form, with smooth
whorls, long-slitted mouth, and very prominent lips, and (2) Pty-
chostoma, resembling Plewrotoma by the peculiar slit on its mouth
and by the lines of growth taking the form of the letter V on the
sides of its smooth polished whorls. Dr. Laube describes 117 species,
among which 22 are new. [Count M. |

ALPHABETICAL INDEX

TO THE

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 Wood, section at Plumstead
Common and, 435.

Aberdeen, dead littoral shells in the
bed of the German Ocean, forty
miles from the coast of, 260.

Aberdeenshire, section at King Ed-
ward, 274, 275.

Acanthodes from the coal-shales of
Longton, Sir P. G. Egerton on a
new species of, 468.

Acanthodes Wardi, 468.

Adams, Dr. A. L., on bones of fos-
sil Chelonians from the ossifer-
ous caves and fissures of Malta,
594; on the discovery of remains
of Halitherium in the Miocene de-
posits of Malta, 595.

Aichmodus, diagrammatic restoration
of the head of, 304.

Affinities of Eozoon Canadense, Dr. W.
B. Carpenter. on the, 219.

of Platysomus and allied genera,
Dr. J. Young on the, 301.

Age of the submerged forest-beds of

_ Porlock Bay, 9.

Agnostus Moret, 487.

Albany and Boston conglomerate,
Michigan, section from the Pewa-
bic lode to the, 453.

Aldborough, section from Orford to
Thorpe near, 21.

Alethopteris Grandini, 157.

grandis, 157.

heterophylla, 157.

lonchitica, 157.

— muricata, 157.

nervosa, 157.

pteroides, 157.

Serlii, 157.

VOL, XXII.

Alresford Creek, Essex, section at the
railway viaduct over, 562.

America, Carboniferous formations of
Eastern, 97; cycles in the Palxo-
zoic age in Kastern, 102.

Ammonites Dunravenensis, 81.

Suttonensis, 81.

Amphicentrum, diagrammatic restora-
tion of the head of, 304.

Amphicentrum granulosun, 306.

Amygdaloid, felspathic, of Ayrshire,
520.

Anatina precursor, var. Pylensis, 88.

Ancillaria lamellata, 579.

ae Lower Miocene deposits of,
973.

Angular detritus of Porlock Bay, 6.

Animals in the Coals of the South
Joggins, genera of, 126.

Annelid-tubes in the Laurentian rocks
of Canada, sketches illustrating sup-
posed, 609.

Anniversary Address of the President,
xxx-cll. See also Hamilton, W. J.,
Esq.

Annual Report, i.

Annularia galioides, 152.

Anomia socialis, 85.

Antholithes pygmea, 149.

— khabdocarpi, 149.

—, sp., 150.

sguamosa, 150.

Antigua, 574.

Antiquity of Man in Ecuador, 567.
Antwerp, crag-beds of, 229.
Araucarites gracilis, 146.

Arca consobrina, 293.

filicata, 583.

— inequilateralis, 293.

INDEX TO THE PROCEEDINGS.

Arca Nox, 283.

Trinitaria, 588.

Ardennais, cailloux, 247.

Ardmore and Youghal trough, lower
limestone shale of the, 333.

Arrigle Brook, section from Knockto-
pher to, 328.

Asphaltic bed, Trinidad, foraminifera
from the Tertiary, 592,

Astarte Duncant, 87.

Asterophyllites in the coal-formations
of the South Joggins, 135.

Asterophyllites equisetiformis, 152.

foliosa, 152.

grandis, 152.

, sp. 152.

trinervis, 152.

Athyris subtilita, 40.

Atlantis hypothesis, 585.

Australia. Petroleum coal-seams in
New South Wales, 435, 439.

Avicula-contorta series, 69.

Ayrshire, Mr. J. Geikie on the meta-
morphic Lower Silurian rocks of
Carrick, 513.

Babbacombe to Watcombe,coast-section

from, 466.
Bagey Point, 346.
Ballea across Myrtle Hill, section from,
35.

Ballinhassig, section near, 337.

Bandon, 335.

Bantry Bay Trough, 541.

Barbadoes, Tertiary deposits of, 578.

Barnwell, bones from the drift of, 476 ;
shells from the drift of, 477.

Barus, Kashmere, plan of part of the
district on the right bank of the Jhe-
lum river, near, 34; section on the
right bank of the Jhelum river, near,
33

Barus and Reshpur, Kashmere, section
along a spur from Wasterwan, be-
tween, bl.

Basement-bed of the London Clay, 412.

Bauerman, H., Hsq., on the Copper-

. mines of the State of Michigan, 448.

Bavaria, species of Hryon from the
Tias and Oolite of, 494.

Beach at Sangatte, 253.

Beinertia Gepperti, 159.

Belgium, Mr.
Austen on the Kainozoic formations
of, 228.

Berehaven Promontory, 343.

Berg, Crag-beds at, 235.

Bermuda, Tertiary deposits of, 579.

Bilberry Hill, section across, 354.

Blackheath and Woolwich, section at, -

435.

R. A. C. Godwin-:

Bluntisham, list of fossils from the
drift of, 471.

Bolderberg, Tertiary deposits of the,
236.

Bones from the drift of Barnwell,
476; of fossil Chelonians from the
ossiferous caves and fissures of
Malta, 594.

Bos Urus, 391.

Boston conglomerate, Michigan, sec-
tion from the Pewabic lode to the
Albany and, 453.

Boulder clay of the Fenland, 479.

Boulders of Caithness, glaciation of
the rocks and, 268.

Bournda, New South Wales, oil-bear-
ing deposits of, 447.

Brachiopodacollected by Capt. Godwin-
Austen in the Mustakh Hills, Thibet,
Mr. T. Davidson, on some Carboni-
ferous, Jurassic, and Cretaceous (?),
35; in the valley of Kashmere, Mr. T.
Davidson on the Carboniferous, 39.

Brachiopoda from Trinidad, Mr. T.
Davidson on Tertiary, 296; Mr. R.
J. L. Guppy on Tertiary, 295.

Brecciiform rocks of Ayrshire, 524. -

Bridgend, Keuper near, 72; Rheetic
beds near, 71.

Brine, Commander L., on the fe0dut
volcanic disturbances in the neigh-
bourhood of Santorino, 319.

Brissus dimidiatus, 301.

Bristow, Mr. H. W., on supposed re-
mains of the Crag on the North
Downs, near Folkestone, 553.

British Crab, oldest known, 493; Oxen,
Mr. W. Boyd Dawkins, on the fos-
sil, 391.

Brodie, The Rey. P. B., on a section
of Lower Lias and Rhetic-beds,.
near Wells, Somerset, 93.

Bulchamp and Waneford Crag-pits re-~
latively to theChillesford clay,section
showing the position of the, 540.

Burragorang, New South Wales, oil-
bearing rocks of, 443.

Butley Crag, 544.

Cailloux Ardennais, 247.

Caithness, list of Mollusca whose shells
are found in the glacial drift of, 278 ;
Mr. T. F. Jamieson on the glacial
phenomena of, 261; sketch map of,
263. :

Calamites in the coal-formations of:
the South Joggins, 135.

Calamites arenaceus, 151.

canneformis, 151.

Cistii, 151.

dubius, 151.

-INDEX TO THE PROCEEDINGS.

Calamites nodosus, 151.

Nova-scotica, 151.

ramosus, 151.

— Suckovii, 151.

Voltzii, 151.

Calamodendron in the coal-formations
of the South Joggins, 134.

Calamodendron approximatum, 149.

obscurum, 149.

Calne railway-station, Wilts, section
of Trail at, 556.

Cambridge, section of a pit in Vic-
toria Road, 561.

Campine sand, 250.

Canada, supposed burrows of worms

_ in the Laurentian rocks of, 608.

Canal-system of Hozoon Canadense, 199.

Cancellaria Barretti, 289.

levescens, 289.

Moorei, 289.

won Coal in New South Wales, 435,

Canterbury, section in the neighbour-
of, 434.

Cape Clear, 340.

Carboniferous Brachiopoda from the
Mustakh Hills, Thibet, 35; from
the valley of Kashmere, 39.

Carboniferous formations of Nova
Scotia and New Brunswick, 97.

Carboniferous Glyptodipterines, Dr. J.
Young on some new genera of, 596.

Carboniferous plants, rate of growth
of, 141.

Carboniferous rocks of the valley of
Kashmere, Capt. H. Godwin-Austen
on the, 29.

Carboniferous Slate(or Devonian rocks)
and the Old Red Sandstone of South
Treland and North Devon, My. J.
Beete Jukes on the, 320.

Cardinia ingens, 86.

Suttonensis, 86.

Cardiocarpum bisectum, 165.

Jfluitans, 165.

, sp., 165.

Cardita? rhomboidalis, 87.

scabricostata, 293.

Cardium castum, 582.

Haitense, 293.

inconspicuum, 293,

lingua-leonis, 293.

Caribean area, paleontology of the,
970.

Carpenter, Dr. W. B., on the struc-

_ ture and affinities of Hozoon Cana-
dense, 219.

Carrick, Ayrshire, metamorphic Lower
Silurian rocks of, 513.

Carrigboy, 335.

Cassidaria sublevigata, 287,

Cassis monilifera, 287.

sulcifera, 286.

Cattle, relation of Bos wrus to the do-
mestic races of, 401.

Caulopteris, sp., 159.

Cercomya ledeformis, 581.

Cerithium plebecum, 290.

Chalk, junction of the Thanet Sand
and the, 402, 405 ; list of fossils from
the beds between the London Clay
and the, 422.

Chama arcinella, 294.

Chambers of Zozoon Canadense, 209.

Chancama, Ecuador, section of the
Point at, 569.

Charcoal, tissues in Mineral, 140.

Cheirotherian footprint from the Keu-
per sandstone of Daresbury, Cheshire,
Prof. W. C. Williamsom on a, 534.

Chelonians from the ossiferous caves
and fissures of Malta, Dr. A. Leith
Adams on bones of fossil, 594.

Chemical characters of Grenville Eo-
zoonal ophite, 187.

Chemnitzia, sp., 88.

Chillesford beds, list of shells from
the, 545.

Chillesford Olay, section showing the
position of the Bulchamp and Wang-
ford Crag-pits relatively to the, 540;
of the Thorpe Crag-pit relatively to
the, 539.

Chillesford Clay or Loam, Rev. O.
Fisher on the relation of the Nor-
wich or Fluvio-marine Crag to the,
19.

Chillesford Church, Suffolk, section of
Trail in a pit east of, 556.

Chondrosteus, Dr. J. Young on the
affinities of, 596.

Chonetes? Austeniana, 44.

Hardrensis, var. Thibetensis, 36.

levis, 44.

Cidaris Melitensis, 299.

Cisseis astericus, 584.

Clarke, The Rev. W. B., on the occur
rence and geological position of oil-
bearing deposits in New South Wales,
439.

Classification of the ‘‘ Lower London
Tertiaries,” 414.

Clay, Chillesford,19; spaces formerly
occupied by selenite in the London,
13.

Clypeaster ellipticus, 299.

Coal, Dr. J. W. Dawson on the con-
ditions of the deposition of, 95.

Coal-formations of Nova Scotia and
New Brunswick, 96.

INDEX TO THE PROCEEDINGS.

Coal-shales of Longton, new species of
Acanthodes from the, 468.

Coast-section from Babbacombe to
Watcombe, 466.

Colchester, section in a ditch on ie
Tendring Hundred Railway, near,
562. .

Colo and Grose rivers, New South
Wales, oil-bearing rocks of, 446.
Colley Creek, Liverpool Plains, New
South Wales, Petroleum coal-seams

at, 435, 440.

Columbella ambiqua, 288.

gradata, 288.

Comeragh Mountains, section across
the, 328,

Coniferous trees in the coal-forma-
mation of the South Joggins, 127.

Coniston flags, 483; limestone, 484.

Connemara, metamorphic rocks of,
509.

Conus gracilissimus, 288.

granozonatus, 287.

— interstinctus, 288.

planiliratus, 287.

solidus, 287.

stenostoma, 287.

Co Mountain, section across,

41.

Copper Harbour to Lac la Belle, Mi-
chigan, section from, 456.

Copper-mines of the State of Michigan,
Mr. H. Bauerman on the, 448.

Copper, origin of, 459.

Coralline Crag, BAL.

Corals from the Sutton Stone, Dr. P
Martin Duncan on the, 8&9.

Corbula vieta, 580.

wiminea, 293.

Cordaites in the coal-formations of the
South Joggins, 139.

Cordaites borassifolia, 164.

simplex, 164.

Cork and Midleton trough, lower lime-
stone shale of the, 3383.

Cork, Old Red Sandstone of N orth, 330.

Countesbury rocks, 3.

Crab, from the For rest Marble, iWelanes:
bury, Wilts, Mr. H. Woodward on
the oldest known British, 493.

Crag-beds of Antwerp, Mr. R. A. C.
Godwin-Austen on the, 229.

Crag, Mr. W. Whitaker on the out-
liers of Sand on the North Downs
which have been classed with the,
430; Mr. 8. V. Wood on the struc-
ture of the Red, 538; on the North
Downs, near Folkestone, Mr. H. W.
Bristow on ees remains of the,
553.

Crag-sand and Thee capping a hill
east of Louvain, section showing, 235.
Crag-sea area, map showing the extent
of the, 240; Mr. R. A. C. Godwin-
Austen on the conditions of the, 238.
Crag to the Chillesford Clay, relation
of the Norwich, 19.
Cretaceous (?) Brachiopoda from the
Mustakh Hills, Thibet, 38.
Crustacea from the Forest Marble,
Malmesbury, Wilts, 493; from the
Lias and Oolite of England and
Bavaria, 494 ; from the Moffat shales,
Dumfriesshire, 503; in the coal-
formations of the SouthJoggins, 144,
Crystalline felstones of Ayrshire, 525
Cuba, Tertiary deposits of, 579.
Cumana, Upper Miocene i a of,
576.

Cycles, geological, 101.

Cyclopteris (Aneimites) Acadica, 153.

antiqua, 154.

— fimbriata, 154.

heterophylla, 153.

hispida, 145.

—— (Neuropteris) ingens, 154,

oblata, 154.

— (N europteris) obliqua, 154.

oblongifolia, 154.

Cyclostrema bicarinata, 291.

Cyperites, sp., 149.

Cyprina normalis, 87.

Cytherea (Circe) carbasea, 292.

— juncea, 582.

(Callista) planivieta, 292.

Dadoxylon Acadianum, 145,

annulatum, 146.

antiquius, 146:

——— materiarium, 145,

Daresbury, Cheshire, Cheirotherian
footprint from the Keuper sand-
stone of, 534.

Davidson, T., Esq., on the Brachio-
poda collected in 'Thibet and Kash-
mere, by Capt. Godwin-Austen, 35.'

Dawson, Dr. J. W., on supposed bur-
rows of worms in the Laurentian
rocks of Canada, 608; on the con-
ditions of the deposition of Coal,
more especially as illustrated by
the Coal-formation of Nova Scotia
and New Brunswick, 95.

Dawson, R., Esq., on the occurrence
of dead littoral shells in the bed of
the German Ocean, forty miles from
the coast of Aberdeen, 260.

Dawkins, W. B., Esq,, on the fossil
British Oxen. Part I. Bos Urus,
Ceesar, 391.

Decigaia, M., on the recent volcanic

INDEX TO THE PROCEEDINGS.

disturbances in the neighbourhood
of Santorino, 318.

Delenda, A., Esq., on the recent vol-
canic disturbances in the neighbour-

_ hood of Santorino, 318.

Dendroptychius, 601 , sketch of a scale
of, 597.

Dentalium dissimile, 292.

Deposition of coal, physical condi-
tions attending the, 98.

Devon, geological structure of North,
346.

Devonian fossils, 365.

Devonian rocks (or Carboniferous
Slate) and the Old Red Sandstone
of South Ireland and North Devon,
Mr. J. Beete Jukes, on the, 320.

Devonshire, valleys and valley-gravels
of, 465.

Dewick, E.8., Esq., on land and fresh-
water shells from the drift of Barn-
well, 477.

Diagram illustrating the motion of a
pebble in a plastic medium, 559;
the succession of formations in North
Devon, 369 ; representing the struc-
ture of the beds between the base of
the Red Crag and the base of the
Upper Drift (Boulder-clay), 548.

Diagram-section across Kent from the
Tertiary Escarpment to the Weald,
435; across North Devon, 360; to
show the general relations of the
formations in Trinidad, 572.

Diagrammatic restorations of the heads
of Amphicentrum, Platysomus, Aich-
modus, and Pycnodus, 304,

Dictyopteris obliqua, 156.

Diestien deposits near Antwerp, 232.

Dingle beds, 344.

Dioritic rocks of Ayrshire, 526.

Diplotegium retusum, 164.

Discina Kashmeriensis, 45,

Discinocaris Browniana, 504.

Domestic races of cattle, relation of
Bos Urus to the, 401.

Donations to the Library, ix., 46, 170,
372, 610; Museum, viii.

Dosinia cyclica, 582.

Downs, outliers of sand on the North,
430; supposed remains of the Crag
on the North, 553.

Drift-gravel at Hitchin, Herts, faults
in the, 565.

Drift of Belgium, glacial, 249; Caith-
ness, 263; New South Wales, 444;
of the Fenland, Mr. Harry Seeley
on the gravels and, 470.

Dulverton, 347; section east of, 348.

Dumfriesshire, new genus of Phyllo-

podous Crustacea from the Moffat
shales, 503.

Duncan, Dr. P. Martin, on some spaces
formerly occupied by Selenite, in
the Lower Eocene clays of the Lon-
don basin; with remarks on the
origin and disappearance of the
mineral, 12; on the corals of the
Sutton Stone, 89.

Duncormick, Wexford, section at, 323.

Dunkerron, 343.

Dunkitt House to Mount Misery,
Waterford, section from, 326.

Dunraven, coast-section from Sutton
to, 75%

Dunster, 349.

Echinoderms from the West Indies,
Mr.R. J. L. Guppy on Tertiary, 207.

Echinolampas lycopersicus, 300.

ovume-serpentis, 300.

semitorbis, 299.

Echinometra acufera, 299.

Echinoneus cyclostomus, 301.

Ecuador, Lieut.-Col. E. St. John
Neale on the discovery of new gold-
deposits in the district of Esmeral-
das, 593; Mr. J. S. Wilson on the
antiquity of man in, 567; on the
geology of the Pacific coast of, 567.

Egerton, Sir P. de M.G., on a new
species of Acanthodes from the Coal-
shales of Longton, 468.

Elie, 280.

Endogenites, 166.

England and France, Mr. A. Tylor on
the valley-gravels of part of, 463.
England, species of Eryon from the

Lias and Oolite of, 494.

Hocene clays of the London basin,
Dr. P. Martin Duncan on some
spaces formerly occupied by Sele-
nite in the, 12.

Eocene formations of the West Indies,

570.

Teor rock, Profs. W. King and
es 3 OS Rowney on the so-called, 185.

Eozoon Canadense, canal- -system of,
199; Dr. W. B. Carpenter on the
structure and affinities of, 219; Profs.
W. King and T. H. Rowney on the
general characters of, 188: proper
wall of, 191; sarcode-chambers of,
209 ; stolon-passages of, 207.

Epidermal tissue of plants in mineral
charcoal, 141.

Equisetites curta, 151.

Errol, 280.

Erycina tensa, 582.

Eryon from the Lias and Oolite of
England and Bavaria, Mr. H. Wood-

INDEX TO THE PROCEEDINGS.

ward on the species of the genus,
494,

Eryon antiquus, 495.

Barrovensis, 495.

- Brodiei, 498.

—— crassichelis, 497,

—— Moorei, 499.

—— Oppeli, 500.

——, sp., 500.

Wilmcotensis, 498.

Esmeraldas, Ecuador, new gold-de-
posits in, 593.

Hssex, section across a furrow of Trail

covered by Warp, at Wivenhoe, 557;.

section of the railway viaduct over
Alresford Creek, 562; section near
Great Bentley church, 555.

Eurynotus, 314.

Fasciolaria semistriata, 288.

Fault in North Devon, probable ex-
istence of a great, 360.

Faults in the Drift-gravel at Hitchin,
Herts, Mr. J. W. Salter on, 565;
in the Lake-country, 485.

Felspar-porphyry of Ayrshire, 520.

Felspathic rocks of Ayrshire, 516.

Fenland, Mr. Harry Seeley on the
gravels and drift of the, 470.

Ferns, vascular bundles of, 140.

Ficula carbasea, 580.

Filices in the coal-formations of the
South Joggins, 135.

Fisher, the Rev. O., on the relation
of the Norwich or Fluvio-marine
Crag to the Chillesford Clay or
Loam, 19.

Fishes in the coal-formations of the.

South Joggins, 144 ; sketches illus-

trating the teeth and scales of some.

new genera of Carboniferous, 597.

Flower, J. W., Esq., on some flint im-
plements lately found in the valley
of the Little Ouse River, near Thet-
ford, 567.

Fluviatile drift of NewSouth Wales, 444.
Fluvio-marine Crag to the Chillesford
Clay or Loam, relation of the, 19.
Folkestone, Mr. H. W. Bristow on
supposed remains of the Cray on

the North Downs near, 553.

Foraminifera from the Tertiary As-
phaltic bed, Trinidad, Prof. T. R.
Jones on, 592.

Forest-beds of Porlock Bay, submer-
ged, 3.

Forest Marble, Malmesbury, Wilts,
Mr. H. Woodward on the oldest
known British Crab from the, 495.

Fort William, 280.

Fossil British oxen, 591; Chelonians

from the ossiferous cayes and fis-
sures of Malta, bones of, 594.

Fossiliferous rocks of the county of
Galway, 506.

Fossils from the Bantry Bay trough,
342; Chillesford beds, 545; Crag at
Walton-on-the-Naze, 542; Drift of
Barnwell, 476; Forest Marble,
Malmesbury, Wilts,493; glacial-drift
of Caithness, 278; Lias and Oolite
of England and Bavaria, 494 ; lime-
stone near Ballea, 336; Lingula-
flags near Tyddyngwladis silver-
lead mine, 505; Lower Miocene de-
pesits of, 574; Manzanilla beds,
Trinidad, 573 ; Moffat shales, Dum-
friesshire, 503; Mustakh Hills, Thi-
bet, 35 ; Mya-bed, 22, 26 ; Oldhaven
beds at Grove Ferry, 416; Silurian
rocks of Galway, 512 ; Tertiary beds
of Jamaica, 285; Upper Miocene
deposits of Cumana, 576; Upper
Miocene deposits of San Domingo,
574; valley of Kashmere, 39; val-
ley of Rocks, 354; in the Coal-
formations of the South Joggins,
125; of Bluntisham, 471; of Hun-
stanton, 473; of March, 473; of
the Caribean Miocene, table show-
ing the affinities of some of the,
588; Crag-beds of Belgium, 242;
Devonian rocks, 865; Lower Lon-
don Tertiaries of Kent, 420; Rhe-
tic beds of South Wales, 79; Sutton

_ and Southerndown series, 81.

Fouqué, M., on the recent volcanic
disturbances in the neighbourhood
of Santorino, 320. J

France,“Mr: A. Tylor on the valley-.
gravels of part of England and,
463. .

Freshwater shells from the Drift of
Barnwell, 477.

Furfooz cave, section of the deposits
at the entrance of the, 248.

Galway, Prof. R. Harkness on the

_ metamorphic and fossiliferous rocks.
of the county of, 506.

Galway Bay, section from Killery.
Harbour to, 507.

Gamrie, 280.

Geographical relations of the Mollusea
of some of the Scottish glacial beds, .
280.

Geological considerations bearing on.
the nature of Eozoonal ophite, 213.

Geological cycles, 101.

Geological position of oil-bearing
rocks in New South Wales, 489.

Geology of Michigan, 449; North.

INDEX TO THE PROCEEDINGS,

Devon, 346; Sinai, 491; South
Treland, 322; the Isle of Man, 488 ;
the Lake-country, 480; the neigh-
bourhood of Porlock, 1; the Pacific
coast of Ecuador, 567.

Conean Ocean, Mr. R. Dawson on the °

- occurrence of dead littoral shells in
the bed of the, 260.

Glacial markings in Caithness, map

_ showing the direction of the, 263.
Glacial Period, place of the Caithness

- Drift in the history of the, 272.

Glacial phenomena of Caithness, Mr.
1’. F. Jamieson on the, 261,

Glaciation of the rocks and boulders
of Caithness, 268.

Glen Roy, Rev. R. Boog Watson on
the marine origin of the Parallel
Roads of, 9.

Glyptodipterines, Dr. J. Young on
some new genera of Carboniferous,
596.

Sa kusien, Capt. H., on the Car-
boniferous rocks of the valley of
Kashmere, with notes on the Bra-
chiopoda ‘collected in Thibet and
Kashmere, by T. Davidson, Esq.,
29; Carboniferous, Jurassic, and
Cretaceous (?) Brachiopoda from the
Mustakh Hills, in Thibet, collected
by, 35; Carboniferous Brachiopoda
from the valley of Kashmere col-
lected by, 39.

Godwin-Austen, R. A. C., Esq., on the
submerged forest-beds of Porlock
Bay, 1; on the Kainozoic forma-
tions of Belgium, 228.

Gold deposits in Esmeraldas, Ecuador,

. Lieut.-Col. EH. St. John Neale on
the discovery of new, 593.

Gravel at Hitchin, Herts, faults.in
the, 565.

Gravel hillocks from Caithness, ab-

' sence of Moraines and, 270.

Grayel-pit, section in the Barnwell,
478.

Gravels and Drift of the Fenland, 470.

Gravels of part of England and France,

. 463.

Gravesend, section between Rochester

- and, 434.

Great Bentley Church, Essex, section
near, 555.

Grenville Eozoonal ophite, characters
of, 187; nature of, 213.

Grose river, New South Wales, oil-
bearing rocks of, 446.

Grove Ferry, fossils from the Old-
haven beds at, 416.

Gryphea athyroides, 583.

Guadeloupe, Tertiary deposits of, 577.

Guppy, R. J. L., Hsq., on the Tertiary
Mollusca of i amaica, 281; on Ter-
tiary Brachiopoda from Trinidad,
295; on Tertiary Echinoderms from
the West Indies, 297; on the rele-
tions of the Tertiary formations of
the West Indies, with a note on a
new species of Ranina from the
Tertiary strata of Trinidad, by H.
Woodward, Esq., and a note on the
Orbitoides and Nummuline of the
Tertiary Asphaltic bed, Trinidad,
by Prof. T. R. Jones, 570.

Halitherium in the Miocene deposits
of Malta, Dr. A. Leith Adams on
the discovery of remains of, 595.

Halonia, sp., 162.

Hamilton, W. J., Esq. (President),
address on presenting the Wol-
laston medal to Sir Charles Lyell,
xxvii; and to Mr. H. Woodward on
handing him the residue of the
Wollaston donation fund, xxix; An-
niversary Address, February 16th,
1866, xxx; Notices of deceased Fel-
lows, "Foreign Members, and Foreign
Correspondents :—Mr, Henr y Chris-
ty, xxx; Sir J. W. Lubbock, xxxi;
Mr. Nicholas Wood, xxxi ; Mr.
Lovell Reeve, xxxiii; Dr. S. P.
Woodward, xxxiv; Mr. G. E. Ro-
berts, xxxvi; Dr. Christian Pan-
der, xxxvi; Dr. Karl yon Raumer,
xxxvii; Dr. C. von Oeynhausen,
xxxix; Dr. Forchhammer, xl; Dr.
Oppel, xl: geological survey of the
United Kingdom, x1; geological sur-
vey of Canada, xli ; Mr. H. Y. Hind
on the geology of New Brunswick,
xliii; geological survey of India,
xlv ; "Messrs. Salter and Blandford
on fossils from Niti, xlvi; Mr. Salter
on British Trilobites, I; Mr. David-
son on British Devonian Brachio-
poda,1; Prof. Phillips on British
Belemnitide, 1; Prof. Owen on
British Liassic Reptilia, li. ; Messrs.
King and Rowney on Lozoon, li;
Dr. Carpenter on Hozoon, lii; Prof.
A. Sismonda on organic remains in
gneiss, lii; M. Barrande on Bohe-
mian Silurian Cephalopoda, hii ;
M. Barrande’s ‘Défense des Co-
lonies,’ li; Prof. T. H. Huxley
and Dr. Wright on reptilian re-
mains from the Kilkenny Coal-
field, ix; M. A. Favre on the Car-
boniferous formation of the Alps,
Ixi; M. Lory on the geology os

INDEX TO THE PROCEEDINGS.

Petit Coeur, lxii; Dr. Gumbel on
the Triassic rocks of Franconia,
lxiii; Dr. Waagen on the Upper
Jurassic formation, lxiv; Dr. F.
Stoliczka on the Gasteropoda of the

Gosau beds, lxv; Prof. Oppel on °

the Tithonic stage, lxv; Dr. Laube
on the fauna of the St. Cassian
beds, Ixvi; M. Jules Martin on the
Rheetic formation, lxvi; Dr. Be-
necke on the Trias and Jura in the
Southern Alps, xvii; M. Renevier
on the Oldenhorn, Ixvii; M. W. A.
Ooster on the fossils of the Swiss
Alps, lxix; Herr von Rath on’ the
copper-mines of Monte Catini, lxix;
Dr. Reuss on the fauna of the Up-
per Oligocene, lxx; Dr. F. Garrigou
on the Quaternary deposits and
bone-caves of the Pyrenees and of
the West of Europe, lxx1i; M.
d’Archiac on the Quaternary fauna,
Ixxiii; Dr. Maack on Lophiodon,
Ixxvi; Count Keyserling and Prof.

- Baer on the transport of erratic
blocks, Ixxvii ; Don Casiano di Pra-
do on the geology of the province
of Madrid, lxxix; M. Crescenzo
Montagna’s ‘ Generazione della ter-
ra,’ Ixxxviii; M. Boué on Turkish
geology, Ixxxviii; Dr. Leidy on the

’ Cretaceous reptiles of North Ame-
rica, xc; MM. Capellini and Heer
on the leaf-beds of Nebraska, xci;
Mr. Lesley on lignite in iron-ore in
Pennsylvania, xcii; M. Jules Mar-
cou on the Falls of Niagara, xciy ;
Dr. Hochstetter on the geology of
New Zealand, xcv; Mr. J. F. Camp-
bell’s ‘Frost and Hire,” xcvii; breaks
in the succession of strata, c; origi-
nal condition of the earth, ci.

Harkness, Prof. R., on the metamor-
phic and fossiliferous rocks of the
County of Galway, 513.

Harkness, Prof. R., and H. Nicholson,
Esq., on the geology of the Lake-
country, with a note on two species
of Trilobites by J. W. Salter, Esq.,
F.G.8., 480; on the Lower Silurian
rocks of the Isle of Man, 488.

“ Heaves” or “throws” in Penhalls
mine, 535.

Hitchin, Herts, Mr. J. W. Salter on

- faults in the Drift-gravel at, 565.

Hitchin Station, section at, 566.

Holland, the Rev. F. W., on the geo-
logy of Sinai, 491.

Holoptychius, 601.

Hook Head, section of part of, 324.

Hughes, T. M‘K., Fsq., on the junc-
tion of the Thanet Sand and the
Chalk, and of the Sandgate beds
and Kentish Rag, 402. |

Hunstanton, list of marine shells from
the drift of, 474.

Hydrothermal metamorphic action,
530.

Hymenophyllites pentadactyla, 159.

Ilfracombe, 354; sketch of contorted
beds traversed by slaty cleavage
near, 356; sketch of a small anti-
clinal ridge in Rapparee cove, near,
356.

Illawarra shales, New South Wales,
44]

Implements found in the valley of the
Little Ouse River, near Thetford,
Mr. J. W. Flower on some (flint,
567.

Ireland (South) and North Devon,
Mr. J. Beete Jukes on the Carboni-
ferous Slate (or Devonian rocks)
and the Old Red Sandstone of, 320.

Isle of Man, section across, 489.

Iveragh, 343.

Jamaica, Hocene deposits of, 570.

Jamaica, Mr. R. J. L. Guppy on the
Tertiary Mollusca of, 281; on the
Upper Miocene deposits of, 575.

Jamieson, T. F., Esq., on the glacial
phenomena of Caithness, 261.

Jhelum river, near Barus, Kashmere,
plan of part of the district on the
right bank of the, 34; section on
the right bank of the, 33.

Joggins, fossils in the coal-formations

-of the South, 125.

Joggins, Logan’s section of the South,

105

Jones, Prof. T. R., on the Orbitoides
and Nummuline of the Tertiary
asphaltic bed, Trinidad, 592.

Junction of the Thanet Sand and the
Chalk, 402, 405; of the Sandgate
beds and the Kentish Rag, 402.

Jukes, J. B., Esq., on’ the Carboni-
ferous Slate (or Devonian rocks)
and the Old Red Sandstone of South
Treland and North Devon, 320.

Jurassic Brachiopoda from the Mus-
takh Hills, Thibet, 37.

Kaimeni Islands, documents relating
to the recent volcanic disturbances
at the, 318.

Kainozoic formations of Belgium, Mr.
R. A. C. Godwin-Austen on the,
228.

Kashmere, Capt. H. Godwin-Austen
on the Carboniferous rocks of the

INDEX TO THE PROCEEDINGS.

- valley of, 29; Mr. T. Davidson on
the Carboniferous Brachiopoda col-
lected by Capt. Godwin-Austen in
the valley of, 39.

Keene, W., Esq., on the brown can-
nel, or petroleum, coal-seams at
Colley Creek, New South Wales,
435.

Keiss harbour, Caithness, section at,
266.

Kent, Diagram section across, 435;

~ Mr. W. Whitaker on the ‘“ Lower

- London Tertiaries” of, 404.

Kentish Rag, junction of the Sandgate
beds and, 402.

Kerry, Old Red Sandstone of South,
330.

Keuper, near Bridgend, 72; of Dares-
bury, Cheshire, Cheirotherian foot-
print from the, 534.

Keweenau Point, Michigan, mines of,

. 485.

Khoonmoo, Kashmere, section across
the entrance of the ravine above the
village of, 34; section near, 32.

Kilchattan, 280.

Kilkenny, Old Red Sandstone of, 327.

Killery Harbour to Galway Bay, sec-
tion from, 507.

Kiltorcan Hill, section across, 328.

King, Prof. W., and Prof. T. H. Row-
ney on the so-called Hozoonal rock,
185.

King-Edward, Aberdeenshire, 280;
section at, 274, 275.

Kinsale, Old Head of, 339.

Knockadoon and Sheeps Head anti-
clinal, 335.

Knocktopher to Arrigle Brook, section
from, 328.

Knorria Sallonii, 164.

Lac la Belle, Michigan, section from
Copper Harbour to, 456.

Lake-basins in New Zealand, Mr. W.
T. Locke-Travers on the formation
of, 254.

Lake-country, Prof. R. Harkness and
Mr. H. Nicholson on the, 480.

Land-animals in the coal-formations
of the South Joggins, 145.

Land-shells from the drift of Barn-
well, 477.

Latirus infundibulum, 288.

Laurentian rocks of Canada, Dr. J.
W. Dawson on supposed burrows
of worms in the, 608.

Lepidodendron in the coal-formations
of the South Joggins, 137.

Lepidodendron aculeatum, 162.

binerve, 161.

:

Lepidodendron clypeatum ?, 162.

—— corrugatum, 169.

decurtatum, 161.

dichotomum, 161.

dilatatum, 161.

—— elegans, 161.

—— gracile, 161.

—— Harcourtii, 162.

personatum, 162.

—— Pictoense, 160.

—— plicatum, 162.

—— plumarium, 162.

rimosum, 161.

selaginoides, 162.

, sp., 161.

—— tumidum, 161.

—— undulatum, 161.

Lepidophloios in the coal-formations
of the South Joggins, 138.

Lepidophloios Acadianus, 163.

parvus, 163.

platystigma, 164.

prominulus, 163.

tetragonus, 164.

Lepidophyllum intermedium, 163.

—— lanceolatum, 163.

—— majus?, 163.

——, sp., 163. :

trinerve ?, 163.

Lepidopleuridz, Dr. J. Young on the
suborder, 315.

Lepidostrobus longifolius, 162.

——, sp., 162.

squamosus, 162.

trigonolepis, 163.

—— variabilis, 162.

Lewisham, section in the neighbour-
hood of, 435.

Lias and Rhetic beds near Wells,
Somersetshire, Rev. P. B. Brodie
on a section of Lower, 93.

Lias of South Wales, 79.

eer species of Kryon from the,

Library, donations to the, ix, 46, 170,
372, 610.

Lima angusta, 83.

—— Dunravenensis, 83.

—— planicostata, 83.

—, sp., 84.

subduplicata, 83.

tuberculata, 82.

Limestone and serpentine in Ayr-
shire, association of, 530.

Lingula-flags, Mr. J. Plant on Pri-
mordial fossils from the, 505. :

Lisoughter, Hozoonal ophite of, 510.

List of bones from the drift of Barn-

well, 476; of fossils from the beds
between the London Clay and the

INDEX TO THE PROCEEDINGS.

Chalk, with their range upward in-
to the basement bed of the London
Clay, into the London Clay, and
into the beds above the London
Clay, 422; from the drift of Blun-

tisham, 471; from the Lingula-.

flags near Tyddyngwladis silver-
lead mine, 505; from the West
Indies, 574; of land and fresh-
water shel]s from the drift of Barn-
well, 477; of marine shells from
the drift of March, 473; of Hun-
stanton, 474; of Mollusca whose
shells are found in the glacial
drift of Caithness, 278; of shells
from the Mya-bed, 22, 26; of
species of Mollusca from the Crag
at Walton-on-the-Naze, 542; from
the Tertiary beds of Jamaica, 28);
of the characteristic fossils of the
Crag-beds of Belgium, 242; of the
fossils from the Oldhaven beds at
Grove Ferry, 417; of the Rhetic
beds of South Wales, 79.

Lithological character of the Old Red
Sandstone and Carboniferous Slate,
changes in the, 344.

Little Ouse River, near Thetford, flint
implements found in the valley of
the, 567.

Littoral shells in the bed of the Ger-
man Ocean, 260.

Liverpool plains, New South Wales,
petroleum coal-seams at Colley
Creek, 435, 440.

Llandeilo flags, Dumfriesshire, Mr. H.
Woodward on a new genus of Phyl-
lopodous Crustacea from the Mof-
fat shales, 503.

Lloyd, St. Vincent, Esq., on the re-
cent voleanic disturbances in the
neighbourhood of Santorino, 318.

Locke-Travers, W. T. L., Esq., on the
formation of lake-basins in New
Zealand, 254.

Loss of Belgium, 251.

Logan, Sir W. E., section of the South
Joggins coal-field, 105.

Lonchopteris tenuis, 156.

London basin, spaces formerly occu-
pied by selenite in the Lower
Eocene clays of the, 12.

London Tertiaries of Kent, Mr. W.
Whitaker on the Lower, 404.

London, sections near, 435.

Longitudinal section along the valley
of Watcombe, 466 ; of Marychurch
valley, 466; of the Central Mine,
Michigan, 457,

Longton, Sir P. G. Egerton on a new

species of Acanthodes from the coal-
shales of, 468.

Loodoo, Kashmere, section on the
south side of the Vihi valley, near
the village of, 35.

Louvain, Crag-beds and Rupellien
clay near, 235; section showing
Crag-sand and shingle capping a
hill east of, 235.

Lower Carboniferous formations of
Nova Scotia and New Brunswick,
97; London Tertiaries of Kent, 404;
Miocene formations of the West In-
dies, 571; Silurian rocks of Car-
rick, Ayrshire, 513; of the Isle of
Man, 488; of the Lake-country,
480; of Wexford, 323.

Lucina Pennsylvanica, 292.

Lyell, Sir C., award of the Wollaston
medal to, xxvii.

Lynmouth to Simonsbath, section
from, 353.

Lynton, 350.

Mactrinula macescens, 581.

Madreporaria from the Sutton Stone,
89

Malea camura, 287.

Malmesbury, Wilts, fossil crab from
the Forest Marble, 493.

Malta, Dr. A. Leith Adams on bones
of fossil Chelonians from the ossi-
ferous caves and fissures of, 594;
on remains of Halitherium in the
Miocene deposits of, 595.

Man, evidence in the Barnwell gravel
of the existence of, 477.

Man in Ecuador, Mr. J. S. Wilson on
the antiquity of, 567.

Man (Isle of), Prof. Harkness and
Mr. H. Nicholson on the Lower
Silurian rocks of the, 488. ~

Manzanilla beds, ‘Trinidad, fossils.
from the, 573.

Map of Caithness, showing the bound-
ary of the dark-grey drift, and the
direction of the glacial markings,
263; of parts of the provinces of
Nelson and Marlborough, new Zea-
land, 255; of the district of Vihi,
Kashmere, 30; of the neighbour-
hood of Porlock, 2; showing the
extent of the Crag-sea area, 240.

March, list of marine shells from,
473; section at, 472.

Marginella coniformis, 288.

Marine origin of the Parallel Roads
of Glen Roy, 9; silt of Porlock
Bay, 5.

Marychurch valley, longitudinal sec-
tion of, 466. ;

INDEX TO THE PROCEEDINGS,

Megalichthys, 606 ; sketch of a scale —

of, 597.

Megaphyton in the coal-formations of
the South Joggins, 136.

Megaphyton humile, 160.

magnificum, 159.

Melanopsis capula, 580.

Mesolepis scalaris, 313.

Wardi, 318.

Metallic minerals of Michigan, 451.

Metamorphic and fossiliferous rocks
of the county of Galway. Prof. R.
Harkness on the, 506; Lower Si-
lurian rocks of Carrick, Ayrshire, 513.

Metamorphism, hydrothermal, 513.

Michigan, Mr. H. Bauerman on the

- copper-mines.of, 448.

Middle Coal-formation of Nova Scotia
and New Brunswick, 97; Lias of
South Wales, 79.

Midleton and Cork trough, lower
limestone shale of the, 333.

Millstone-grit of Nova Scotia and New
Brunswick, 97.

Milton Lane, near Wells, section at, 94.

Mineral characters of Grenville Ko-
zoonal Ophite, 187 ; charcoal, tissues
in, 140; condition of organic re-
mains in the Woolwich beds, 13.

Mineral range, Michigan, section of
the Trappean belt of the, 452.

Mines of the State of Michigan, 448.

Miocene, age of the Caribean, 577;
deposits of Malta, remains of Hali-
therium in the, 595; formations of
the West Indies, 571; of Jamaica,
relationships of the, 281.

Mitra Henekeni, 288.

Mizen Head, 340.

Modiola imbricato-radiata, 87.

Moffat shales (Llandeilo flags), Dum-
friesshire, Mr. H. Woodward on a
new genus of Phyllopodous Crus-
tacea from the, 503.

Mollusea from the Chillesford beds,

- 545; from the Crag at Walton-on-
the-Naze, 542 ; of Jamaica, Tertiary,
281; of some of the Scottish glacial
beds, geographical relations of the,
280; of the glacial Drift of Caith-
ness, list of, 278.

Moraines and gravel-hillocks from
Caithness, absence of, 270.

Mortehoe, 357.

Mount Calabash, Trinidad,
from Nariva Swamp to, 573.

Mount Misery, Waterford, section
from Dunkitt House to, 326.

Murex Domingensis, 288.

Museum, donations to the, viii,

section

Mustakh Hills, Thibet, Brachiopoda
from the, 35.

Mya-bed, shells from the, 22, 26.

Myrtle Hill, section from Balleaacross,
33D.

Nariva Swamp to Mount Calabash,
Trinidad, section from, 573.

Nassa solidula, 579.

Natica mammillaris, 291.

phasianelloides, 291.

—— Pylensis, 89.

—-—- suhclausa, 290.

sulcata, 291.

Nattai river, New South Wales, oil-
bearing rocks of the, 442. —

Neale, Lieut.-Col. E. St. J., on the
discovery of new gold-deposits in
the district of Esmeraldas, Ecuador,
593.

Nelson and Marlborough, New Zea-
land, sketch map of parts of the
provinces of, 255.

Neritina Woodwardi, 291.

Neuropteris acutifolia, 155.

attenuata, 155.

auriculata, 155.

—— conjugata, 155.

—— cordata, 154.

cyclopterotdes, 155.

—— dentata, 155.

—— flexuosa, 155.

—— gigantea, 155.

heterophylla, 155.

—— Loshii, 155.

perelegans, 154.

rarinervis, 154,

Soretii, 155.

Voltzii, 155.

New Brunswick, Dr. J. W. Dawson
on the Coal-formation of, 95.

New South Wales, Rey. W. B. Clarke.
on the occurrence and geological
position of oil-bearing rocks in, 439;
Mr. W. Keene on the examination
of brown cannel, or petroleum, coal-
seams at Colley Creek, Liverpool
Plains, 435.

New Zealand,
basins in, 254. :

Nicholson, H., Hsq., and Prof. R.
Harkness on the geology of the
Lake-country, with a note on two
species of Trilobites by J. W.
Salter, Esq., F.G.S., 480; on the
Lower Silurian rocks of the Isle of
Man, 488.

Neggerathia dispar, 153.

—— flabellata, 153.

North Devon, geological structure of,
345. .

formation of lake-

INDEX TO THE PROCEEDINGS.

North Downs, outliers of sand on the,
430 ; supposed remains of the Crag
on the, 553.

Norwich or Fluvio-marine Crag to the
Chillesford Clay or Loam, Rev. O.
Fisher on the relation of the, 19.

Nova Scotia, Dr. J. W. Dawson on
the Coal-formation of, 95.

Nummuline of the Tertiary asphaltic
bed, Trinidad, Prof. T. R. Jones on
the Orbitoides and, 592.

Odontopteris Schlotheimii, 155.

—— subcuneata, 155.

Oil-bearing rocks in New South Wales,
geological position of, 439.

Oldhaven beds, Mr. W. Whitaker on
the, 412.

Old Red Sandstone of South Iveland
and North Devon, Mr. J. Beete
Jukes on the Carboniferous Slate
(or Devonian rocks) and the, 320.

Oliva reticularis, 288.

Ontonagon district, Michigan, 458.

Oolite, species of Eryon from the, 494.

Ophite, characters of Grenville Ho-
zoonal, 187; nature of Hozoonal,
213.

Orbitoides and Nummuline of the
Tertiary asphaltic beds, Trinidad,
Prof. T. R. Jones on the, 592.

Orford to Thorpe near Aldborough,
section from, 21.

Origin of Copper, 459; of Selenite,
15; of the Parallel Roads of Glen
Roy, 9.

Orthis, sp., 36.

Ostrea levis, 84.

multicostata, 84.

Oxen, Mr. W. Boyd Dawkins on the
fossil British, 391.

Pacific coast of Ecuador, geology of
the, 567.

Paisley, 280.

Paleinachus longipes, 494.

Palxontology of the Caribean area,
570.

Paleopteris Acadica, 159.

Sa Ele ae, NDS)

Paleozoic age in Eastern America,
cycles in the, 102; rocks near Por-
lock, 3.

Panoramic sketch of the hills around
the Vihi valley, Kashmere, 31.

Paragenesis of minerals, 459.

Parallel Roads of Glen Roy, Rev. R.
Boog Watson on the marine origin
of the, 9.

Patella Suttonensis, 88.

Pecopteris abbreviata, 158.

—— acuta, 158.

Pecopteris squalis, 158.

arborescens, 157.

— Bucklandi, 158.

—— cyathea, 158.

—— decurrens, 159.

—— longifolia, 158.

oreopteroides, 158.

—— Pluckenetii, 159.

—— plumosa, 158.

polymorpha, 158.

—— rigida, 158.

—— Sillimani ?, 158.

—— texniopteroides, 158.

—— unita, 158.

villosa, 158.

Pecten Etheridgit, 81.

—— exasperatus, 294.

inequalis, 294.

——, sp., 82.

Suttonensis, 81.

Pectunculus acuticostatus, 293.

pennaceus, 293.

Peltocaris aptychoides, 504.

Penhalls mine, Mr. J. W. Pike on
some remarkable ‘“ heaves” or
“throws” in, 535.

Perna? Ramsayi, 86.

Persona sinillima, 288.

Petroleum Coal-seams in New South
Wales, 435, 439.

Pewabic lode to the Albany and Bos-
ton conglomerate, Michigan, section
from the, 453; mine, section of the
Pewabic lode in the end of the
130-fm. level, 454.

Phacops Nicholsoni, 486.

Phos elegans, 290.

- Moorei, 290.

Phyllopodous Crustacea from the Mof-
fat shales, Dumfriesshire, 505.

Phyllopteris antiqua, 157.

Physical conditions attending the de-
position of Coal, 98.

Pickwell Down, 357.

Pike, J. W., Esq., on some remarka-
ble “heaves” or “throws” in Pen-
halls Mine, 535.

Pinna insignis, 85.

Pinnularia capillacea, 153.

erassa, 153.

—— ramosissima, 153.

Plan of part of the district on the
right bank of the Jhelum river, near
Barus, Kashmero, 34; of the ridge
near Zebanwan, Kashmere, 32.

Plant, J., Esq., on the discovery of
Primordial Fossils in the Lingu-
la-flags in the neighbourhood of
Tyddyngwladis Silver-lead Mine,
505.

INDEX TO THE PROCEEDINGS,

Plant-growthin Porlock Bay, submerg-
ed surface of, 5,

Plants in the coals of the South Jog-
gins, genera of, 126; rate of growth
of Carboniferous, 141.

Platysomus and allied genera, Dr. J.
Young on the affinities of, 301;
diagrammatic restoration of the
head of, 304.

Platysomus parvulus, 308.

Pleurotoma Barretti, 290.

—— consors, 289.

Jamaicense, 290.

-—— venustum, 289.

Plicatula acuminata, 86.

intusstriata, 86.

Plumstead Common and Abbey Wood,
section at, 435.

Polder-mud of Belgium, 251.

Porcupine Mountains, Michigan, 453.

Porlock Bay, Mr. R. A. C. Godwin-
Austen on the submerged forest-
beds of, 1.

Post-glacial period in Caithness, 276.

Priest's Leap, section from Reenydo-
negan Lough across Coomhola
Mountain to, 341.

Primordial fossils in the neighbour-
hood of Tyddyngwladis silver-lead
mine, Mr. J. Plant on, 305.

Productus Cora, 43.

Humboldtii, 43.

— levis, 44.

longispinus ?, 43.

scabriculus, 48.

—— semireticulatus, 56, 43.

——, sp., 44.

spinulosus?, 44.

striatus ?, 44.

« Proper wall” of Hozoon Canadense,
191.

Psaronius, sp., 159.

Pychnophyllum in the coal-forma-
tions of the South Joggins, 139.

Pyenodus, diagrammatic restoration
of the head of, 304.

Pyle, South Wales, Rheetic beds near,
70.

Quebrada of Chancama, Ecuador, 569.

Queenstown, 335.

Ranella crassa, 288.

Range of Bos Urus in space and time,
397.

Ranina from the Tertiary strata of
Trinidad, Mr. H. Woodward on a
new species of, 591.

Ranina porifera, 591.

Rapparee Cove near Ilfracombe, sketch
of a small anticlinal ridge in, 356.

Reading and Woolwich beds, 409.

Red Crag, Mr. 8. V. Wood on the
structure of the, 538.

Reedy Creek, New South Wales, oil-
bearing rocks of, 444.

Relations of the divisions of the
‘«Lower London Tertiaries,” 418.
Reshpur, Kashmere, section along a
spur from Wasterwan between

Barus and, 31.

Reenydonegan Lough across Coom-
hola Mountain to Priest’s Leap,
section from, 341.

Rhabdocarpus insignis, 150.

, sp., 150.

Rhetic beds in South Wales, Mr. E.
B. Tawney on the western limit of
the, 69 ; near Wells, Somerset, Rev.
P. B. Brodie on a section of Lower
Lias and, 93.

Rhizodopsis, 596; sketches of a scale
of, 597.

Rhizodus, 599; sketch of a tooth and
a scale of, 597; Dr. J. Young on
the scales of, 317.

Rhomboptychius, 604; sketches of a
tooth and a scale of, 597.

Rhynchonella Barumensis, 42.

—— Kashmeriensis, 42.

— Katonensis, 37.

pleurodon, var. Davreuxiana, 36.

, sp., 38.

Rochester and Gravesend, section be-
tween, 434.

Rochester (Upnor), section at 434.

Rocks, Lynton, section across the val-
ley of, 351.

Rowney, Prof. T. H., and Prof. W.
King, on the so-called Eozoonal
rock, 185,

Rupellien clay of Schelle, 234.

Sables de la Campine, 250.

Salter, J. W., Esq., on faults in the
Drift-gravel at Hitchin, Herts, £65;
on two species of Trilobites from
the Lower Silurian rocks of the
Lake-country, 486.

San Domingo, Upper Miocene deposits
of, 574.

San mage Trinidad, section at,
57

Sandgate beds and Kentish Rag, Mr.
T. M‘Kenny Hughes on the junc-
tion of the, 402.

Sangatte beach, Mr. R. A. C. Godwin-
Austen on the, 253.

Santorino, documents relating to the
recent volcanic disturbances in the
neighbourhood of, 318.

Sarcode-chambers of Eozoon
dense, 209,

Cana-

-INDEX TO THE PROCEEDINGS.

Scalariform vessels, 140.

Scaldésien deposits near Antwerp, 231.

Scales of new genera of Carboniferous
fishes, sketches illustrating the teeth
and, 597.

Scales of Rhizodus, Dr. J. Young on
the, 317.

Schelle, Rupellien clay of, 254.

Schizaster Scillze, 301.

Scotland, relation of the Caith-
ness Drift to that of the rest of,
270.

Scottish glacial beds, table showing
the geographical relations of groups
of Mollusca whose shells occur in
some of the, 280.

Scrabster Harbour, Caithness, section
at, 264.

Scrobicularia-Crag, 544.

Section across a furrow of Trail cover-
ed by Warp, Wivenhoe, Essex, 557 ;
Bilberry Hill, 334; Kent, from the
Tertiary Escarpment to the Weald,
435; Kiltorcan Hill, from Knock-
topher to Arrigle Brook, 328; North
Devon, 360; the Comeragh Moun-
tains, 328; the entrance of the ra-
vine above the village of Khoonmoo,
Kashmere, 34; the Isle of Man,
489; the Valley of Rocks, 351;
along a spur from Wasterwan, be-
tween Barus and Reshpur, Kash-
mere, 31; the valley of Watcombe,
466; at Blackheath and Woolwich,
435; Duncormick, Wexford, 323;
Hitchin Station, 566; Keiss Har-
bour, Caithness, 266 ; King-Edward,
Aberdeenshire, 274, 275; March,
472; Milton Lane, near Wells, 94;
Plumstead Common and Abbey
Wood, 435; Rochester (Upnor),
434; San Fernando, Trinidad, 571] ;
Scrabster Harbour, Caithness, 264;
Shottenden Hill, 484; the foot of
a ridge from Zebanwan, Kashmere,
32; the railway viaduct over Alres-
ford Creek, Essex, 562; Wick Bay,
Caithness, 265; between Rochester
and Gravesend, 434; from Babba-
combe to Watcombe, 466; Ballea
across Myrtle Hill, 335; Copper
Harbour to Lac la Belle, Michigan,
456; Dunkitt House to Mount
Misery, Waterford, 326; Killery
Harbour to Galway Bay, 507; Lyn-
mouth to Simonsbath, 353; Nariva
Swamp to Mount Calabash, Trini-
dad, 573; Orford to Thorpe, near
Aldborough, 21; Reenydonegan
Lough across Coomhola Mountain

to Priest’s Leap, 341; Sutton to
Dunraven, 75; the Pewabic Lode
to the Albany and Boston Conglo-
merate, Michigan, 453; in a ditch
on the Tendring Hundred Railway
near Colchester, 562; Penhalls
mine, 537; the Barnwell grayel-
pit, 478; the neighbourhood of
Canterbury, 434; of Lewisham,
435; of Sittingbourne, 434;
near Ballinhassig, 337; Khoon-
moo, Kashmere, 32; London, 435 :
of a furrow which crosses the
Tendring Hundred Railway near
Great Bentley Church, Essex, 555 ;
a pit in Victoria Road, Cambridge,
561; Lower Lias and Rhetic beds
near Wells, Somersetshire, 93;
Marychurch valley, 466; part of
Hook Head, 324; Southerndown
cliff, 75; the Central Mine, Michi-
gan, 457; the deposits at the en-
trance of the Furfooz cave, 248;
the Pewabic Lode in the end of the
180-fm. level, Pewabic Mine, 454;
the point at Chancama, Heuador,
569; the South Joggins Coal-field,
105 ; the Trappean belt of the mine-
ral range, Michigan, 452; Trail at
Calne railway-station, Wilts, 556; at
Woking, Surrey, 556; in a pit east
of Chillesford church, Suffolk, 556;

near Villa Farm, Tendring Hun-

dred Railway, BOT ; on the right
bank of the Jhelum river, near
Barus, Kashmere, 33 ; the south sidé
of the Vihi valley, near the village
of Loodoo, Kashmere, 35; Thurso
Water, near Thurso, 267; showing
Crag-sand and shingle capping a
hill east of Louvain, 235 ; the posi-
tion of the Bulchamp and Wangford
Crag-pits relatively to the Chilles-
ford Clay, 540; of the Thorpe
Crag-pit relatively to the Chilles-
ford Clay, 539; Warp cut off by
erosion of a stream, 563; the gene-
ral relations of the formations in
Trinidad, 572.

Sections illustrating supposed Annelid-
tubes in the Laurentian rocks of
Canada, 609.

Seeley, He Esq., on the Gravels and
Drift of the Fenland, 470.

Selenite in the Lower Eocene Clays of
of the London basin, Dr. P. Martin
Duncan on some spaces os
occupied by, 12.

Serpentine of Ayrshire, 527; Conne-
mara, 509. :

goa FS

INDEX TO THE PROCEEDINGS.

Sheeps Head and Knockadoon Head
anticlinal, 335.

Shells from the Chillesford beds, 545 ;

- Crag at Walton-on-the-Naze, 542;
drift of Barnwell, 477; Hunstan-
ton, 474; March, 473; the Mya-
bed, 22, 26; the Tertiary beds of
Jamaica, list of, 285; in the bed of
the German Ocean, forty miles from
the coast of Aberdeen, Mr. R. Daw-
son on the occurrence of dead lit-
toral, 260; Coal-formations of the
South Joggins, 143; drift of Caith-
ness, state of the, 267; of some of
the Scottish glacial beds, geographi-
cal relation of the, 280; the Crag-
beds of Belgium, 242; the glacial
drift of Caithness, list of, 278.

Shingle-beach of Porlock Bay, 4.

Shottenden Hill, section at, 434.

Sigillariz in the coal-formations of
the South Joggins, 128.

Sigillaria(Favularia) Bretonensis, 148.

Brownit, 146.

— catenoides, 147.

Dournansii, 148.

— (Favularia) elegans, 146.

— elongata, 147.

—— eminens, 148.

flexuosa, 147.

— Knorrii, 148.

levigata, 147.

— (Clathraria) Menardi, 147.

organum, 147.

pachyderma, 147,

— planicosta, 147.

reniformis, 146.

- —— (Rhytidolepis) Saullii, 146.

— (——) Schlotheimiana, 146.

—— (——) scutellata, 146.

, 8p., 147.

striata, 147.

—— (Asolanus) Sydnensis, 147.

(Fayularia) tessellata, 146.

Silurian rocks of Carrick, Ayrshire,
Mr. J. Geikie on the Metamorphic
Lower, 513; the Isle of Man, 488 ;
me Lake-country, 480; Wexford,

Simonsbath, section from Lynmouth
to, 353.

Sinai, Rev. F. W. Holland on the
geology of, 491.

Sittingbourne, section in the neigh-
bourhood of, 434.

Skeleton (intermediate) of Hozoon Ca-
nadense, 212. .

Sketches illustrating the teeth and
scales of some new genera of Car-
boniferous Fishes, 597,

Sketch map of Caithness, showing the

- boundary of the dark-grey drift, and
the direction of the glacial markings,
263; parts of the provinces of Nel-
son and Marlborough, New Zealand,
255; the district of Vihi, Kashmere,
30; the neighbourhood of Porlock, 2.

Sketch of a small anticlinal ridge in
Rapparee Cove, near Ilfracombe,
356; contorted beds traversed by
slaty cleavage, half-a-mile east of
Ilfracombe, 356 ; panoramic, of the
hills around the Vihi valley, Kash-
mere, 31.

Skibbereen, 535.

Skiddaw slates, 480.

Solarium quadriseriatum, 291.
Solenites, 166.

Somerset, Lower Lias and Rheetic beds

near Wells, 93.

Somme, valley-gravels of the, 464.

Southerndown Cliff, vertical section
Obs pat
Southerndown series, 74.

South Ireland, Upper Palzeozoic rocks

of, 322.
South Wales, western limit of the
Rheetic beds in, 69.

Spaces formerly occupied bySelenite, 12.

Spencer Mountains, New Zealand,
sketch map of parts of the provinces
of Nelson and Marlborough in the
neighbourhood of the, 255.

Sphenophyllum emarginatum, 152.
erosum, 152.

longifolium, 152.

— saxifragifolium, 152.

Schlotheimii, 152.

Sphenopteris artemisizfolia, 156.
Canadensis, 156.
decipiens, 156.

gracilis, 156.

— hymenophylloides, 156.

Jatior, 156.

—- Lesquereuxii, 156.

microloba, 156.

—— munda, 156.

obtusiloba ?, 156.

Spirifera Barusiensis, 42.
Kashmeriensis, 41.
Moosakhailensis, 41.

Rajah, 40.

, sp., 36.

— Vihiana, 41.

Spirorbis carbonarius, 144.

clymenioides, 584.

Sporangites in the coal-formations of

the South Joggins, 139. ©

glabra, 165.

papillata, 165.

INDEX TO THE PROCEEDINGS,

Sternbergia, 165. :

oe of Eozoon Canadense,
207.

Stones imbedded in the drift of Caith-
ness, character of the, 266.

Stony Creek, New South Wales, oil-
bearing rocks of, 439.

Stigmaria ficotdes, 148.

cee 602; sketch of a tooth of,
a97.

Streptorhynchus crenistria, 42.

, sp., 49.

Strombus bifrons, 287.

pugilis, 287.

Structural characters of Grenville Ko-
zoonal ophite, 187.

Structure and affinities of Eozoon Ca-
nadense, 219.

Structure of the Red Crag, 538.

Submerged forest-beds of Porlock Bay,
156:

Succession of formations in
Devon, diagram of the, 369.

Suffolk, section of Trail in a pit east of
Chillesford church, 556.

Surrey, section of Trail at Woking,
556.

Sutton Crag, 543.

Sutton series, 72.

Sutton stone, Dr. P. Martin Duncan
on the corals from the, 89; Mr. EH.
B. Tawney on the position of the,
69, 77.

Sutton to Dunraven, coast-section from,

North

Syringodendron, sp., 148.

Systeme Diestien, 232; Scaldésien, 251.

Table of cycles in the Paleozoic age in
Eastern America, 102; fossils com-
mon to the districts north and south
of the central band of Old Red Sand-
stone in North Devon, 364; Mol-
lusca whose shells are found in the

glacial drift of Caithness, 278; the ©

species of the genus Eryon occurring
in the Lias and Oolite of England
and Bavaria, 501 ; showing the affi-
nities of some of the fossils of the
Caribean Miocene, 588; the geogra-
phical relations of groups of Mol-
lusca whose shells occur in some of
the Scottish glacial beds, 280; the
range of the fossils of the Rhetic
beds of South Wales, 79; the rela-
tive frequency of occurrence of genera
of plants and animals in the coals
of the South Joggins, 126.
Tawney,E. B., Esq., on the western limit
of the Rheetic beds in South Wales,
and on the position of the Sutton

stone, with a note on the Corals by
Dr. P. Martin Duncan, 69.

Teeth and scales of new genera of Car-
boniferous fishes, sketches illustra-
ting the, 597.

Tendring Hundred Railway, sections
on the, 555, 557, 562.

Terebra inzqualis, 290.

Terebratula Austeniana, 35.

carneoides, 296.

lecta, 296.

sacculus, 40.

— Thibetensis, 37.

-—-— Trinitatensis, 296.

Terrestrial surface of Belgium, ancient,”
252.

Tertiaries of Kent, Mr. W. Whitaker
on the Lower London, 404.

Tertiary Brachiopoda from Trinidad,
295 ; escarpment to the Weald, dia-
gram section across Kent from the,
435; formations of Belgium, Mr.
R. A. C. Godwin-Austen on the,
228: formations of the West Indies,
Mr. R. J. L. Guppy on the rela-
tions of the, 570; Mollusca of Ja-
maica, Mr. R. J. L. Guppy on the,
281.

Thanet beds, Mr. W. Whitaker on the,
405; Sand and the Chalk, Mr. T.
M‘Kenny Hughes on the junction
of the, 402.

Theoretical remarks on the gravels
and drift of the Fenland, 479.

Theory of metamorphism, 513.

Thetford, Mr. J. W. Flower on some
flint implements found in the valley
of the Little Ouse river, near, 567.

Thibet, Mr. T. Davidson on some Car-
boniferous, Jurassic, and Cretace-
ous (?) Brachiopoda collected by
Capt. Godwin-Austen in the Mus-.
takh Hills, 35.

Thickness of the rocks of North Devon,
361.

Thorpe Crag-pit relatively to the Chil-
lesford Clay, section showing the
position of the, 539.

Thorpe near Aldborough, section from
Orford to, 21.

Throws in Penhalls mine, 535.

Thurso Water, Caithness, section on
the, 267.

Tracey, 358.

Trail, sections of, 556, 557.

Trappean belt of the mineral range,
Michigan, section of the, 452.

Trigonocarpum avellanum, 150.

Trigonocarpum Hookeri, 150,

intermedium, 150,

INDEX TO THE PROCEEDINGS.

Trigonocarpum minus, 150.

Neeggerathi, 150.

rotundum, 150.

sigillarie, 150.

Trilobites, Mr. J. W. Salter on two
species of, 486.

Trimmer, Mr., Rev. O. Fisher on the
Warp of, 553.

Trinidad, Lower Miocene deposits of,
571; Mr. R. J. L. Guppy on Ter-
tiary Brachiopoda from, 295; Upper
Miocene deposits of, 575.

Trochotoma, sp., 89.

Tryon, Commander G., on the recent

- volcanic disturbances in the neigh-
bourhood of Santorino, 319.

Turbo castaneus, 291.

Turon drift, New South Wales, 446.

Turritella, sp., 89.

tornata, 580.

Tyddyngwladis silver-lead mine, Pri-
mordial fossils from near, 505.

Tylor, A., Esq., on the interval of time
which has passed between the for-
mation of the Upper and Lower
valley-gravels of part of England
and France, 463.

Upnor, section at, 434.

Upper Coal-formation of Nova Scotia
and New Brunswick, 96; Miocene
deposits of the West Indies, 574;
Palzozoic rocks of Wexford, 322.

Urus, characters of the, 392.

Valley-gravels of part of England and
France, Mr. A. Tylor on the interval
of time which has passed between
the formation of the Upper and
Lower, 463. :

Valley of Rocks, section across the, 351.

Valley of the Little Ouse River, near
Thetford, Mr. J. W. Flower on some
flint implements found in the, 567.

Vegetable tissues in mineral charcoal,
140.

Venus paphia, 292.

Walli, 581.

Woodwardi, 292.

Vermetus papulosus, 292.

Vertical section at Blackheath and
Woolwich, 485; Plumstead Com-
mon and Abbey Wood, 485; Ro-
chester (Upnor), 434; Shottenden
Hill, 484; between Rochester and
Gravesend, 434; in the neighbour-
hood of Canterbury, 434; Lewis-
ham, 435; Sittingbourne, 434; near
London, 435; of Southerndown
cliff, 75.

Vibi, Kashmere, sketch map of the
district of, 30; rough panoramic

VOL. XXII,

sketch of the hills around the valley
of, 31; near the village of Loodoo,
Kashmere, section on the south side
of the, 38.

Villa Farm, Tendring Hundred Rail-
way, section of Trail near, 557.

Volcanic disturbances in the neigh-
bourhood of Santorino, documents
relating to the recent, 318.

Waldheimia Blanfordi, 38.

Wales, western limit of the Rheetic
beds in South, 69.

Walton-on-the-Naze, list of species of
Mollusca from the Crag at, 542.

Wangford Crag-pit relatively to the
Chillesford Clay, section showing
the position of the, 540.

Warp (of Mr. Trimmer), its age and
probable connexion with the last
geological events, Rev. O. Fisher on
the, 553. :

Wasterwan, Kashmere, section along a
spur from, 51.

Watcombe, coast-section from Babba-
combe to, 466; longitudinal section
along the valley of, 466.

Waterford, Old Red Sandstone of
South, 330; section from Dunkitt
House to Mount Misery, 326.

Watson, Rev. R. Boog, on the marine
origin of the Parallel roads of Glen
Roy, 9.

Weald, diagram section across Kent,
from the Tertiary escarpment to the,
435.

Wells, Lower Lias and Rhetic beds
near, 93.

West Indies, Mr. R. J. L. Guppy on
Tertiary Echinoderms from the,
297 ; on the relations of the Tertiary
formations of the, 570.

Wexford, Upper Paleozoic rocks of,
322.

Whitaker, W., Esq., on the ‘‘ Lower
London Tertiaries” of Kent, 404.
Wick Bay, Caithness, section at, 265.
Williamson, Prof. W. C., on a Cheiro-
therian foot-print from the base of
the Keuper sandstone of Daresbury,

Cheshire, 534.

Wilson, J. S., Esq., on the geology of
the Pacific coast of Ecuador, and on
some evidence of the antiquity of
Man in that region, 567.

Wilts, fossil crab from the Forest Mar-
ble, Malmesbury, 493; section of
Trail at Calne railway station, 556.

Wivenhoe, Essex, section across a fur-
row of Trail covered by Warp at,
507.

INDEX TO THE PROCEEDINGS.

Woking, Surrey, section of Trail at,
556.

Wollaston Donation Fund, award of
the, xxix.; Medal, award of the,

BS cq gtn

Woolwich and Reading beds, Mr. W

- Whitaker on the, 409.

Woolwich beds, mineral condition of
organic remains in the, 13; spaces
formerly occupied by selenite in the,
12

Woolwich, section at Blackheath and,
435.

Wood, 8. V., Esq., on the structure
of the Red Crag, 538.

Wood, 8. V., jun., Hsq., on a diagram
representing the structure of the beds
between the base of the Red Crag
and the base of the Upper Drift
(Boulder-clay), 546.

Wood-cells in mineral charcoal, 140.

Woodward, H., Esq., award of the
Wollaston Donation Fund to, xxix. ;
on a new species of Ranina from
the Tertiary strata of Trinidad, 591 ;
on the oldest known British crab

(Paleinachus longipes) from the
Forest Marble, Malmesbury, Wilts,
493; on a new genus of Phyllopo-
dous Crustacea from the Moffat
Shales (Llandeilo Flags), Dumfries-
shire, 503; on the species of the
genus ryon, Desm., from the Lias
and Oolite of England and Bavaria,
494.

Worms in the Laurentian rocks of .
Canada, Dr. J. W. Dawson on sup-
posed burrows of, 608.

Youghal and Ardmore trough, Lower
Limestone shale of the, 333.

Young, Dr. J., on new genera of Car-
boniferous Glyptodipterines, 596 ;
on the affinities of Chondrosteus, Ag.,
596; on the affinities of Platyso-
mus and allied genera, 301; on the
scales of Rhizodus, 317.

Zebanwan, Kashmere, plan of the ridge
near, 32; section at the foot of a
ridge from, 32.

Zoological features of the Crag-sea
area, 241.

THE END.

Printed by TAYLOR and FRANCIS, Red Lion Court, Fleet Street.

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