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LIBRARY OF
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For the Promotion of Research in
PALEOBOTANY and PALEOZOOLOGY
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SMITHSONIAN INSTITUTION
WASHINGTON, D. C.
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: THE
§
GEOLOGICAL SOCIETY OF LONDON.
EDITED BY
THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.
Quod si cui mortalium cordi et cure sit non tantum inventis heerere, atque iis uti, sed ad ulteriora
penetrare ; atque non disputando adversarium, sed opere naturam vincere; denique non belle et probabiliter
opinari, sed certo et ostensive scire; tales, tanquam veri scientiarum filii, nobis (si videbitur) se adjungant.
—Novum Organum, Prefatio.
VOLUME THE TWENTY-SEVENTH.
1871.
LONDON :
LONGMANS, GREEN, READER, AND DYER.
PARIS: FRIED. KLINCKSIECK, 11 RUE DE LILLE; F, SAVY, 24 RUE HAUTEFEUILLE.
LEIPZIG: T. 0. WEIGEL.
SOLD ALSO AT THE APARTMENTS OF THE SOCIETY.
; ° MDCCCLXXI.
Ltst
OF THE
OFFICERS -
OF THE
GEOLOGICAL SOCIETY OF LONDON.
WPA AE OPIS LIA
Elected February 17, 1871.
!
RIAD
Prestvent.
Joseph Prestwich, Esq., F.R.S.
Wice-Presivents.
Sir P. de M. G. Egerton, Bart., M.P., F.R.S. | Sir Charles Lyell, Bart., F.R.S.
Prof. T. H. Huxley, LL.D., F.R.S. Prof. John Morris.
Secretaries.
- John Evans, Esq., F.R.S., F.S.A. | David Forbes, Esq., F.R.S.
Foreign Secretary.
Prof. D. T. Ansted, M.A., F.R.S.
Creasurer.
J. Gwyn Jeffreys, Esq., F.R.S. —
COUNGEIL.
Prof. D. T. Ansted, M.A., F.R.S. . Prof. T. H. Huxley, LL.D., F.R.S.
W. B. Carpenter, M.D., F.R.S. J. Gwyn Jeffreys, Esq., F.R.S. & L.S.
W. Carruthers, Esq., F.R.S., F.L.S. Sir Charles Lyell, Bart., D.C.L., F.R.S.
W. Boyd Dawkins, Esq., M.A., F.R.S. C. J. A. Meyer, Esq.
Prof. P. Martin Duncan, M.B. Lond., F.R.S. | Prof. John Morris.
Sir P. de M. G. Egerton, Bart., M.P., F.R.S. | Joseph Prestwich, Esq., F.R.S.
John Evans, Esq., F.R.S., F.S.A. Prof. A. C. Ramsay, LL.D., F.R.S.
J. Wickham Flower, Esq. R. H. Scott, Esg., M.A., F.R.S.
David Forbes, Esq., F.R.S. Prof. Tennant, F.C.S.
Captain Douglas Galton, C.B., F.R.S. Rev. Thomas Wiltshire, M.A., F.L.S.
R. A. C. Godwin-Austen, Esq., F.R.S. Henry Woodward, Esq., F.Z.S.
J. Whitaker Hulke, Esq., F.R.S.
Assistant-Secretarp, Librarian, anv Curator.
W. S. Dallas, Esq., F.L.S.
Clerk.
Mr. W. W. Leighton.
Library Assistant.
Mr. F. H. Waterhouse.
TABLE OF CONTENTS.
PART I.—ORIGINAL COMMUNICATIONS.
Page
Bonney, Rey. T.G. On the Formation of “Cirques,” and their Se
Bearing upon Theories attributing the Excavation of Alpine
Valleys mainly to the Action of Glaciers......./.........+-: 312
Bropiz, Rev. P. B. On the “ Passage-beds”’ in the neighbourhood
of Woolhope, Herefordshire, and on the Discovery of a new
Species of Hurypterus and some new Land-Plants in them .... 256
CaRRUTHERS, WILLIAM, Esq. On some supposed Vegetable Fos-
SIS) 0 (CHILD Od IEEE) 4 ole nne eso ee ain ab Og oo ADO aC nUn omar S 443
Dawkins, W. Boyp, Esq. On the Discovery of the Glutton (Gulo
(FERGIE) SUAU BS CTL OVE Sar is ec ety Pee Peete SS eR Ae a 406
Dawson, J. W., LL.D. On the Structure and Affinities of Sigdlaria,
Calamites, and Calamodendon. (With 4 Plates.) ............ 147
. On New Tree-Ferns and other Fossils from the Devonian.
GUY At aR aE aS) FE ea RIS Sigur re crak arse bivlete ins Nee ae 8 269
D’ORvETA, M. On some points in the Geology of the Neighbour-
Hoodie Valaoata(( Wathia Plates). estes germ © eccicels syrsisie oi 109
Drayson, Lieut.-Col., R.A. On the probable Cause, Date, and
Duration of the Glacial Epoch of Geology. [Abstract.] ...... 232
Duncan, Prof. P. Martrm. On a new Species of Coral from the
Prema ra oot NVpeuld inn call Cle Ao) is atic ode naancnishal tdears's ais ajan als slays 369
On the Persistence of Caryophyllia cylindracea, Reuss, sp.,
a Cretaceous species of Coral, in the Coral-fauna of the Deep Sea 484
Egerton, Sir Puitre Grey, Bart. On a new Chimeroid Fish
from the Lias of Lyme Regis (Ischyodus orthorhinus, 3).
(CLOG) 9 EA ENESS) Yo Sea sae Sa ea A eco oe ae aR HIS Aico crys 275
Fatrpank, F. Royston, M.D. On the Discovery of a “ Bone-bed ”
in the Lowest of the “Lynton Grey Beds,” North Devon.
Peli leroralliy steak ar nayneee ths tava tals apes oo) aetna 'y sauahoRenetetede a aynral a « 33
iv TABLE OF CONTENTS.
Pa
GRIKIE, ARCHIBALD, Esq. On the Tertiary Volcanic Rocks of the
British Islands.—First Paper. (With a Plate.)............4. 279
GinFILian, G., Esq. On the Diamond-districts of the Cape of Good
Blgpe.. | Albstractsl) o 0c re ease sue leis «= lei one) mrnis efeney seen
Green, A. H., Esq. Notes on the Geology of part of the County of
Donegal. ~ \PAStraeb ses Pe she ske eet meine alee fe elelede tel eley att leateteinan 449
Grey, Grorcr, M.D. Remarks on some Specimens from South
Africa, with Notes by Prof. T. Rupert Jones. [Abstract.].... 49
GRIESBACH, CHARLES LupotF, Esq. On the Geology of Natal in
South Attica. / (Vahl 2Pla tess) 2 )cisr)s) elas erates een 53
Harkness, Prof. R., and H. Hicxs, Esq. On the Ancient Rocks of
the St. David’s Promontory, South Wales, and their Fossil
Contents. With Descriptions of the New Species, by H. Hicks,
Bsqs (With 2 Plates.) (gr ee o cee aele ascent out ens eteee ee 384
HawxsHaw, J. C., Esq. Notes on the Peat and Underlying Beds
observed in the construction of the Albert Dock, Hull.
[ebridoed ees isl stateicaseiaele c se cls abides cesta cake cea ene 237
Herr, Prof. O. On the Carboniferous Flora of Bear Island (lat. 74°30!
IN, Jap [LADS Er BCH: ie cie sre acters oicnedeu tee a canttve| siolane cacao ea il
Herman, W. Doveras, Esq. On Allophane, and an Allied Mineral
found at Northampton pcyyhinale a «js id de) yMee once aetna tet ree 234
Hicxs, Henny, and Prof. R. Harkness. On the Ancient Rocks of
the St. David’s Promontory, South Wales, and their Fossil Con-
tents. With Descriptions of the New Species, by H. Hicks, Esq.
C Wrath: Bla bes) rave us dg acral cactark mers tc etare Siena ele iece rea 384
Hux, J. W., Esq. Note on some Reptilian Fossils from Gozo.... 29
. Note on a large Reptilian Skull from Brooke, Isle of Wight,
probably Dinosaurian, and referable to the genus Iguanodon.
(Wath a Plates) 0. Since ee cents Sie del aeiaitauel ated cree eee 199
. Note on an Ichthyosaurus (I. enthekiodon) from Kimmeridge
Bay, Dorset.’ \(Withia Plate.) 0. <2 semen eiee is eee 440
Note on a Fragment of a Teleosaurian Snout from Kim-
meridge Bay, Dorset. (With a Plate.) ........ Rodeiele So eantugs 442
JamiEson, T. F., Hsq. On the Older Metamorphic Rocks and Granite
Of Bantishines vary. osasilolavoricu sie aera eel aceite 101
Jones, Prof. T. Rupert. See GEorGE Grey, M.D.
Jupp, J. W., Esq. On the Puntield Formation) 52... -s.qceeee 207
Kinasmiiu, T. W., Esq. The probable Origin of Deposits of “ Loess”
in’ North China and) Waster Asia.:.cs. moe oe) e cist eee 376
TABLE OF CONTENTS. v
Losey, J. Logan, Esq. On the Principal Features of the Sitar
graphical Distribution of the British Fossil Lamellibranchiata.. 411
Loan, T., Esq. Memoranda on the most recent Geological Changes
of the Rivers and Plains of Northern India, founded on accurate
Surveys and the Artesian Well-boring at Umballa, to show
the practical application of Mr. Login’s s Theory of the abrading
and transporting power of water to effect such changes. [Ab-
SIMA C ep eee ene et ctah takers NU ane ate Wne MER ena ances d ove 451
Meyer, C. J. A., Esq. On Lower Tertiary Deposits recently ex-
posed at TE ar iV re ene Abe tea 74
Mircueiyi, W. STEPHEN, Esq. Some Remarks on the Denudation
of the Oolites of the Bath District, with a Theory on the Denu-
dation of Oolites generally. [ Abridged. dD Sie Stead Marte en eras 228
Murpuy, JoserpH Joun, Esq. On the Connexion of Volcanic Action
with Changes of Level. [Abstract.] ........ Heperacetes tices 5 108
PRESTWICH, JOSEPH, Esq. On the Structure of the Crag-beds of
Suffolk and Norfolk, with some Observations on their Organic
Remains.—Part I. The Coralline Crag of Suffolk, (With a
eC Mme rem a mete tie eter atin tect ocr sfotever sl af sol nou ea lark ele -s\403 war's) A leha' bhatt 115
Part Il. The Red Crag of Essex and Suffolk.... 326
. Part II. The Norwich Crag and Westleton Beds.
(GV iene I Ailes) lie aia a atawtase aiiats aver cue (6) orate Shatate «dee twilae aigsvale as 453
Ramsay, Prof. A.C. On the Physical Relations of the New Red
Marl, Rheetic Beds, and Lower lias ........0.01.. cece ees 189
On the Red Rocks of England of Older Date than the
—_——_,
Saws, J. G., Esq. Geological Observations on British Guiana.. 419
Scort, Roprrt H., Esq. Notes on the Minerals of Strontian,
Aerie, § 6 5a diocea on eb.6 5 Oe tee Come Doe OU Oath Gicicld vce ec 372
Stow, G. W., Esq. On some Points of South-African Geology.—
Heniyte perros Peace tel ccierer spares: SP eteretel sieliers Syaivien sie wien aitecaraeovare 8 28, 497
ALAN UE sapopatatayrel nics SetaaC te) raid ae sie creds: weaiiella gene 52, 528
ae EIU oslo teee nonmencemoct ole coarcaad 584
Tate, RaupH, Esq. On the Age of the Nubian Sandstone........ 404
TREVELYAN, Sir W. C., Bart. On supposed Borings of Lithodomous
Aielingces “JD NSinaie ml Goes oon cod eatin ae ecimoermioD Mice 231
Wurraker, Witi1aM, Esq. On the Chalk of the Cliffs from Sea-
ford to Eastbourne, Sussex. [Title only.] ...........-..0-. 92
On the Chalk of the Southern Part of Dorset and Devon.. 93
On the Cliff-sections of the Tertiary Beds west of Dieppe
in Normandy, and at Newhaven in Sussex ............0..55- 263
vi TABLE OF CONTENTS.
Page
Woon, 8. V., Jun., Esq. On the Evidence afforded by the Detrital
Beds without and within the North-eastern part of the Valley
of the Weald as to the Mode and Date of the Denudation of
that Valley." CWith!a Plater). si. cata pane cielo oe ryrolinie elie 3
Woopwarp, Henry, Esq. Notes on some new Crustacea from the
Lower Eocene of Portsmouth. (With a Plate.) ............ 90
. Ona New Species of Eurypterus (£. Brodiet), from Perton,
near Stoke: Hdithy Elerefordshire o's). ae)er eee estenet ene 261
Anmuall Report: cisiese°s v's sales aris wiles e aide sein tae eo ae ee i
Aumiversary AGGress | .y.:..2 do: cyeeseleeee wos aetarale erate Meee te ree p.0.0.4
luist'of HoreignMemibers). “ican eisiaetne tee atten ie tee Xvi
listof Moreien’ Correspondentsicy iy. sone cee dee eee xviii
iist-of \Wiollaston’ Medallists: (....-ec ids sete Gees See
Donations to the Library (with Bibliography) .. viii, 34, 162, 357, 549
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.
PLANTS.
Caulopteris antigua. PI. xii. f. 1-3 \ (271
Lockwoodi. Pi. xii. f. 4 ...... | | 270
: i |
xii Ne la percgrenn. EN. | Devonian .........,N. America sreeee] 4 272
Ges Deore Susecossoaquadassaaco:
Neeggerathia gilboensis. Pl. xii. f.8 | | | 273
Rhachiopteris, sp. Pl. xii. f. 7...... y) | ( 273
PROTOZOA.
Protospongia(?)major. Pl. xvi.f. 14-18I|Cambrian ......!St. David's ........- | 401
EcHINODERMATA.
Diadema, sp. PI. iii, f. 13 ....... -....[Cretaceous ......1Natal ..-......... col (Ge
Mo..vsca.
( Brachiopoda.)
Lingulella primeva. P\. xv. f. 13, 14...\Cambrian ...... ISt. David’s ......... | 401
(Lamellibranchiata.)
Area capensis. PI. iii. f. 10......... | ( 66
Astarte, sp. Pl. iii. f, 9 ........000. 67
Cardium denticulatum. PI. iii. f. 12 | l. 4 Natal 67
Pecten amapondensis. PI. iii. f. 7... f Pye pede = RROGe ae aa aed { 66
Pectunculus africanus. PI. iii. f. 8 | | 66
Trigonia Shepstonei. PI. iii. f. 11...) | \ 66
(Pteropoda.)
Theca antiqua. Pl. xvi. f. 13 ......... iCambrian......... ISt. David’s ......... | 400
| ( Gasteropoda.)
Cerithium (Fibula) detectum .. ... | 64
kaffrartum. Pl. iii. f.5 ...... 64
Chemnitzia undosa .......0.......... STE AGEDES Sooo MIEN ccnss9 scrauteg 65
Vill
Name of Species. | Formation. Locality: Page.
Mo..usca (continued).
( Cephalopoda.)
Ammonites Achilles. Pl. v.f.1 ......\Jurassic ......... Malaga ...... coo'see| ams:
Kayei.......... Seanpocnonaced ee aincist Cretaceous ......|Natal ............... 63
——-~ perarmatus, var. catena. Pl.v.f.3)Jurassic ......... Malaga............+s. 113
—rembda. Pl. iii. f. 2,3 ...... 63
Bee So eaiasie CBIR 1 hora Cretaceous ...... Natal’ oc. ccedsessenee 63
Ryos, JEG 6 ts) ecgaonsodqneccoqann »-|JUTASSIC ......00. Malaga ...........- 113
Anisoceras rugatum. PI. iii. f.4......|Cretaceous ...... Natal 7 tac. scsoemes 63
Teudopsis Brodie ....... Beene. cRECOe eS ...|Purbeck .........|Dorsetshire.........| 448
ANNULOSa.
( Crustacea.)
Agnostus cambrensis. PI. xvi. f.11, )
DS Se oseoaoserinocecaonenanemsoounono[s Cambrian St. David’ 400
Conocoryphe Lyellii, Pl. xvi.f. 1-7 {|~~ Dee So aa 399
solvensis. PI. xvi. f. 8 ...... 400
Eurypterus Brodiet ....cscecsovsevecees Silurian ......... Herefordshire ......) 261
Leperditia (?) cambrensis. Pl. xv. i.
UB=H 7 ScceconoondcessoSsoudescosoanen es Cambrian......... St. David’s ......... 401
Microdiscus sculptus. Pl. xvi. 9, 10 400
Paleocorystes glabra. Pl. iv. f.1 ...;/Lower Eocene...|Portsmouth......... 90
iv. ¢ Oe Fopeconystes) Mullert- EI: | Upper Chalk ...|Maestricht ......... 99
Paradoxides Harknessi. Pi. xv. f.
QV egy cisac iia acmtowate vee esesiseseeeis Cambrian...... .../St. David’s ......... 399
Plutonia Sedgwickii. Pl. xv. f. 1-8 399
Psammocarcinus Heriecartii. Pl.iv. f.4.;|Lower Eocene...|France............... 92
Rhachiosoma bispinosa. PI. iv. f. 3 91
cchinaia® ORB fars ak Lower Eocene.../Portsmouth........ 92
VERTEBRATA.
(Pisces.)
Ischyodus orthorhinus. P. xiii. ...... IES Gocoocnnen6onse ILyme Regis......... ] 275
(Reptilia.)
Crocodilus gaudensis ......1.....seeceese ee realsieiecisielaae GOZO cases oeeneness 30
Ickthyosaurus enthekiodon. P\. xvii...|Kimmeridge me Kimmeridge ...... 440
gaudensis ...... steceesca te sasa eset sass ovale sn |(OZO eae ecencnascene 29
Iguanodon (?). Pl. Xi. ..........00eeeeee Wealden ... ..... Isle of Wight ...... 201
Teleosaurus megarhinus. P). xviii. ...|Kimmeridge Clay|Kimmeridge ...... 442
ie bane an or : oe Great Oolite......|Cirencester ......... 447
odtusatus. Pl. xix. f. 1-3 ...... Wealden ......... Isle of Wight ......| 447
sphericus. P\. xix. f. 4-7, 10...|Stonesfield Slate/Stonesfield .... 447
EXPLANATION OF THE PLATES.
PLATE Pace
q, J Mars anv Szcrrons, to illustrate Mr. 8. V. Wood’s paper on
: the Denudation of the Weald Valley ..............c.ccsseeneens
II. aed AnD Srcrions, to illustrate Mr. C. L. Griesbach’s paper
ontthe Geolosyot Nataly se crcccsctranemteseorecncnicctenceence st 70
lr | eee Fosstus rrom Naat, to illustrate Mr. C. L.
ar Griesbach’s paper on the Geology of Natal ...........sceeceseee 70
paper on New Crustacea from the Lower Eocene of Ports-
7 New Eocene Crusracsa, to illustrate Mr. H. Woodward’s
IV.
AIO VEL ester Pea aa eteRieiertos ee seaises selec ctate acces hace seaneicncasacn 92
Ammonites From Mataaa, to illustrate M. d’Orueta’s paper
on the Geology of the Neighbourhood of Malaga ............ 113
PLAN AND SEcTIoNS oF CORALLINE CRAG, to illustrate Mr. Prest-
VI
Vis
wich’s first paper on the Crag-beds of Suffolk and Nor-
HOWE sponpmonoceces wiclesiacislonaremeive cater cmmehtoiaewion ela Seatac aeeiieclucieaise steel 146
VII.
VIIT STERNBERGIZ, CALAMODENDRA, CALAMITES, and SIGILLARLA,
: to illustrate Dr. Dawson’s paper on the structure and
i SVITOMITES OF ACRE (HEAR, sescgonancbcaoooscobonpoan wesunaqsoononce 160
xy, { Rerrmn Sxoxt, to illustrate Mr. Hulke’s paper on a Rep-
tilian Skull from Brooke, Isle of Wight .............c. ccononos AUS
XII Tree Ferns anp Na@ecGeraruta, to illustrate Dr. Dawson’s
; paperon Devonian’ Plants) yos-.c-ms.ssccceess snaeossteneseescieeee 274
XT { Iscuyonpus ortHoruinvs, to illustrate Sir Philip Hgerton’s
meme lb paper ona new Chimeroid Pishs.c<. .c-.cs..ccmeneeen ces veo eons 278
xy, J Views or tre Scir or Era, to illustrate Mr. A Geikie’s paper
1 on the Tertiary Volcanic Rocks of the British Islands ...... 310
XV Lower Camprian Fossits, to illustrate Messrs. Harkness and
XVL Hicks’s paper on the Ancient Rocks of St. David’s Pro-
Pa MM OMUOWYE tac aatass aceon ae ose tacdenehoncs dqucsua cos rescestesedegs age wane 402
IcHTHYOSAURUS ENTHEKIODON, to illustrate Mr. Hulke’s paper
ane on an Ichthyosaurus from Kimmeridge Bay ..................
XVIII TELEOSAURUS MEGARHINUS, to illustrate Mr. Hulke’s paper on
; a Teleosaurus from Kimmeridge Bay ...........0...sseeeeeee eee
XIX SuprosEeD VEGETABLE Fossius, to illustrate Mr. Carruthers’s
ao paper on some supposed Vegetable Fossils .............seeeeee- 448
Xx Srcrions, to illustrate Mr. Prestwich’s third paper on the Crag-
a pedsiomSuirollk andl Nortolkgascncee-crseaeesseecesmecseseee seen 496
We bot 2
re ee
te
ERRATA ET CORRIGENDA.
Page 65, line 12 from bottom, for Bailey read Baily.
”
98, last line, for &c. read and c.
109, head-line and title of paper, for de Orueba read d’Orueta.
111 and 113, head-line, for de Orueba read d’Orueta.
273, line 5 from bottom, for Neggarathia read Neggerathia.
537, deser. of fig. 13, for Palzozic read Paleozoic.
GEOLOGICAL SOCIETY OF LONDON.
ANNUAL GENERAL MEETING, FEB, 17, 1871.
REPORT OF THE CoUNCIL FoR 1870.
Tue Council of the Geological Society, in presenting their Report
for the year 1870, have again to congratulate the Fellows on the
increasing prosperity of the Society.
' The number of new Fellows elected was 58, of whom, however,
only 42 paid their fees before the end of the year, making, with 9
previously elected Fellows who paid their fees in 1870, a total
effective increase of 51 Fellows. Against this must be placed the
loss of 21 Fellows by death, of 5 by resignation, and of 3 removed
from the list on account of non-payment of contributions, making
a total of 29, and thus giving a net increase of 22 ordinary Fellows.
The number of Contributing Fellows is now 533.
The election of 1 Foreign Member and of 2 Foreign Correspon-
dents took place in 1870, and the death of 1 Foreign Member was
announced.
The total number of Fellows and Foreign Members and Corre-
spondents at the end of 1869 was 1222; and at the end of 1870,
1245, -
The Council have much gratification in reporting that, notwith-
standing a very heavy expenditure in illustrations for the Quarterly
Journal of the Society, the Income of the year 1870 exceeded the
Expenditure by £156 Os. 9d.; the total Receipts being £2050, and
the total Expenditure £1867 15s. 8d. Under these circumstances
the Council felt justified in investing a further sum of £200 in the
purchase of £211 7s. 3d. of 3 per cent. Consols.
The Council have to announce the completion of Vol. XXYVI. of
the Quarterly Journal, and the commencement of the publication of
Vol. XXVIT.
They have also to announce that to provide for the increasing cir-
culation of the Quarterly Journal, and in order to be able to present
copies to the Foreign Correspondents, they have decided in future
to print 1500 copies of it, and also to give the authors of papers
published in the Journal 25 separate copies properly made up, in
lieu of the 15 copies which have hitherto been prepared by cutting
up twice that number of sheets of the Journal.
VOL, XXVII. | a
A
il ANNIVERSARY MEETING.
The Council have also to announce that Dr. C. F. Fischer of
Auckland, New Zealand, presented to the Society the remainder of
the copies (in all 291) of a translation made by him of Messrs.
Hochstetter and Petermann’s ‘Geology of New Zealand,’ accom-
panied by an atlas of six maps. The Council decided to ‘sell these
books to' the Fellows at a low price.
The Council have awarded the Wollaston Medal to Prof. A.C.
Ramsay, F.R.S., F.G.S., &c., in recognition of his valuable services
to physical and stratigraphical geology, and with especial reference to
his numerous and original geological essays relating to Wales and
the adjacent counties, and his surveys.of that district. |
The Balance of the proceeds of the Wollaston Fund has been
awarded to Robert Etheridge, Esq., F.G.S., to aid him in prosecuting
his work on the Fossils of the British Islands, stratigraphically
arranged.
The Council have the gratification of reporting that an Appeal
against the Assessment of Parochial Rates was on the 138th of this
month decided by the proper Tribunal in favour of the Society, by
which their total exemption from such imposts has been established.
Report of the Labrary and Museum Committee, 1870-71.
_Lnbrary.
The Standing Library-Committee have continued from time to
time to make additions to the Library by the purchase of such books
as they thought would prove useful to the Fellows; and amongst
those purchased since the last Anniversary Meeting, the following
important works may be cited :—
Berendt’s ‘ Geologie des Kurischen Haffes und seiner Umgebung;’
Blanford’s ‘ Observations on the Geology and Zoology of Abyssinia 3’
C. F. Naumann’s ‘ Elemente der Mineralogie ;’ Landgrebe’s ‘ Mine-
ralogie der Vulcane;’ Percy’s ‘Metallurgy of Lead ; Veith’s
‘ Deutsches Bergworterbuch ;’ Issel’s ‘ Malacologia del Mar Rosso ;?
Zittel’s ‘ Paleontologische Mittheilungen aus dem Museum des
Konigl. Bayerischen Staates;’ Mayr’s ‘Ameisen des baltischen
Bernsteins ;’ Weiss’s ‘ Fossile Flora der jiingsten Steinkohlenforma-
tion und des Rothliegenden im Saar-Rhein-Gebiete ;’ and conti-
nuations of Pictet’s ‘Matériaux pour la Paléontologie Suisse ;?
Schimper’s ‘ Paléontologie Végétale ;? Milne-Edwards’s ‘ ‘Recherches
Anatomiques et Paléontologiques pour servir 4 THistoire des
Oiseaux fossiles de la France;’ Ooster’s ‘ Protozoé Helvetica ;’
Quenstedt’s ‘ Petrefactenkunde Deutschlands Porites Paleontogra-
phica;’. the ‘ Paléontologie Francaise ;’ and Reeve’s ‘ Conchologia
Iconica.’ The cost of books purchased by the Society during the
past year was £37 7s. 11d., and of binding £33 13s. 7d.
A great number of valuable books have been presented to the
Society’ s Library during the past year, including, besides periodicals
and the publications of ‘learned Societies, many separate works of im-
portance, such as :—
‘Gea Norvegica,’ Parts 1-3 (1838-50), from the Royal Norwe-
ANNUAL REPORT, ili
gian University in Christiania; M. L. Lartet’s ‘Essai sur la Géolo-
gie de la Palestine et des Contrées avoisinantes ;’ the fourth and fifth
parts of M. Laube’s ‘Fauna der Schichten von St. Cassian ;’ Prof.
Ansted’s ‘ Physical Geography and Geology of Leicestershire ; the
continuation of M. Barrande’s ‘Systéme Silurien du Centre de la
Bohéme ;’ M. Belgrand’s ‘ Le Bassin Parisien aux Ages Antchistori-
ques ;’ Sir John Lubbock’s ‘ Prehistoric Times ;’ Mr. Seeley’s ‘ Orni-
thosauria, an elementary study of the Bones of Pterodactyles ;’ the
continuation of M. Stoppani’s ‘ Paléontologie Lombarde ;’ M. Eugéne
Kudes-Deslongchamps’s ‘Notes Paléontologiques ;’? Prof. Gould’s
‘Report on the Invertebrata of Massachusetts,’ presented by the
Kditor, W. G. Binney, Esq.; the continuation of Prof. Hall’s « Pale-
ontology of New York;’ and Mr. Safford’s ‘ Geology of Tennessee.’
From Mrs. Hamilton, the widow of the late W. J. Hamilton, Esq. :,
the Society received an immense collection of tracts, with permis-_
sion to select such as might be wanting in the Society’s Library. A
great number of valuable treatises have been thus added to the
Library ; and the Society is deeply indebted to Mrs. Hamilton for
the liberality thus displayed by her,
Many Maps and Plans have been added to the Society’s Collection;
‘they include the Maps of Geological Surveys of Queensland (Cape
River Gold-field and Canal-Creek Diggings), Hesse (Sect. Alsfeld),
Sweden (5 sheets), Prussia and Thuringia (6 sheets), Austria (2
sheets), and Switzerland (8 sheets and a sheet of sections); also
M. Delesse’s ‘ Carte lithologique de ’/Embouchure de la Seine ;’? Mr.
Lapham’s ‘Geological Map of Wisconsin;’? a Sketch-map of the
Geology of New Zealand, by Dr. James Hector; and a geologically
coloured Map of Lundy Island, prepared and presented by N. Whit-
ley, Esq. Prof. yori Dechen’s ‘ Geologische Karte yon Deutschland ’
has been purchased for the Library.
Numerous Maps published by the Ordnance Survey, and Maps,
Charts, and Plans published by the French Dépét de la Marine, have
also been presented; and 2 Maps of South Africa, by Mr. Henry
Hall, have been purchased.
Museum.
The Collections in the Museum remain in good condition, and
several portions of them have been consulted by foreign geologists
during the past year, Very few additions have been made to the
collections, the principal being, numerous specimens of Corals from
the South-Australian Tertiaries, in illustration of Dr. Duncan’s pa-
per and presented by him; and Fossils and Casts of Fossils from
the Newer Tertiaries of Suffolk, presented by E. Ray Lankester,
Esq., in illustration of his paper on, those deposits,
THOS. WILTSHIRE.
J. GWYN JEFFREYS.
WARINGTON W. SMYTH.
ROBERT A. C. GODWIN-AUSTEN.
a 2
iv ANNIVERSARY MEETING.
Comparative Statement of the Number of the Society at the close of
the years 1869 and 1870.
Dec. 31, 1869. Dec. 31, 1870-
Comiponndersjsn ween 2 LONI ox tvaae 218
Contributing Fellows...... OIL 6 » tenis sect 533
Non-Contributing Fellows . AQ ai here 412
1141 1163
Honorary Members ...... ih Pen 3
Foreign Members ........ OO.) yea eee 39
Foreign Correspondents.... DO Tih canna 40
1222 1245
General Statement explanatory of the Alteration in the Number of
Fellows, Honorary Members, dc., at the close of the years 1869
and 1870.
Number of Compounders, Contributing and
Non-contributing Fellows, December 31, 1141
WS 6 Oi reeces ct seas te ere tates ee Nee ae
Add Fellows elected during former year,
pravalonnich mi O) iio s eeadis eel aes ee A
Add Fellows elected and paid in 1870...... 42
1192
Deduct Compounders deceased .........--- 4
Contributing Fellows deceased ...... 9
Non-contributing Fellows deceased .. 8
Contributing Fellows resigned .....- 5
Contributing Fellows removed ...... 3 -
1163
Number of Honorary Members, Foreign
Members, and Foreign coments 81
Mecembersai el SOO hee ws cutee rene
Add Foreign Member elected ...........- 1
Foreign Correspondents elected ...... 2
84
Deduct Foreign Member deceased........ if
Foreign Correspondent elected Fo- i 1
relomuNlemperatecs «1. ve eerie i
— 2
— 82
1245
ANNUAL REPORT. v
Deceased FELLOWS.
Compounders (4).
C. Collier, M.D. Sir F. Pollock, Bart.
The Bishop of Manchester. A. Rogers, Esq.
Resident and other Contributing Fellows (9).
C. W. V. Bradford, Esq. M. C. Morrison, Esq.
E. W. Brayley, Esq. B. B. Orridge, Esq.
H. Hakewill, Esq. . S. Perkes, Esq.
R. Hutton, Esq. C. Sanderson, Esq.
E. Jones, Esq. |
Non-contributing Fellows (8).
C. W. Bigge, Esq. Rey. R. Gwatkin.
E. B. Blackburn, Esq. Capt. L. L. B. Ibbetson.
Rey. C. Erle. J. Walker, Esq.
Rev. J. H. Fisher. G. Woods, Esq.
Foreign Member (1).
Dr. Gustav Bischof.
Fellows Resigned (5).
Hon. J. Abercromby. Capt. Drury Lowe.
Major Arbuthnot. H. A. Ward, Esq.
F. Hill, Esq.
x Fellows Removed (3).
Owen Bowen, Esq. Bassett Smith, Esq.
R. Mills, Esq.
The following Personage was elected a Foreiyn Member during the
year 1870.
Dr. Oswald Heer, of Zurich.
The following Personages were elected Foreign Correspondents during
the year 1870.
Prof. Joseph Szabo, of Pesth.
Prof. Otto Torell, of Lund.
vi ANNIVERSARY MEETING.
The following Persons were elected Fellows during the year 1870.
January 12th.—John Aitken, Esq., Bacup, Manchester; Edward
Allen, Esq., 19 St. Saviourgate, York; Clement Cadle, Esq.,
Gloucester ; Arthur Wyatt Edgell, Esq., Lympstone, Exeter ;
Charles F. Leaf, Esq., Old Change, H.C., and Harrow; and
Samuel Joseph Smith, Esq., 29 Park Road, New Wandsworth,
S.W.
26th.—Thomas Daniel Bott, Esq., 2 Osborne Villas, Talfourd
Road, Peckham, §8.E.; Edwin B. Kemp-Welch, Esq., 3 Beau-
mont Terrace, Bournemouth; James Parkinson, Esq., Sarum
House, Church Road, Upper Norwood, 8.E.; Henry Sewell, Esq.,
Villa del Valle, Mexico; and T. F. W. Walker, Esq., M.A,
6 Brock Street, Bath.
February 9th.—Alexander Murray, Esq., Geological Survey of
Canada, St. John’s, Newfoundland ; and Frederick William Rud-
ler, Hsq., Museum, Jermyn Street, S.W.
23rd. __ Alexander Cig) ale Harding, King’s College, London,
W.C.; Thomas Adair Masey, Hsq., 6 Crown Office Row, Temple,
J dO. 3 "and Samuel Haslett, Hsq., Ann Street, Belfast.
March 9th. —John Alleyne Bosworth, Esq., Humberstone, Leices-
tershire ; Robert Erskine Brown, Esq., Wass, Oswaldkirk, York-
shire ; Major K. H. Sladen, Madras Staff Corps, Church Road,
Upper Norwood, 8.H.; and Henry King Spark, Esq., Green Bank,
Darlington.
23rd.—Frederick Antony Potter, Esq., B.Sc., Cromford, Derby-
shire.
April 13th.—8. W. North, Esq., Castlegate, York.
27th.—Robert Logan Jack, Esq., Geological Survey of Scot-
land, India Buildings, Victoria Street, Edinburgh ; George Alex-
ander Lebour, Esq., Geological Survey of England, Museum,
Jermyn Street, S.W.; Coles Child, Esq., The Palace, Bromley,
Kent ; and Harry Rivington, Esq., 22 Finsbury Square, E.C.
May 1th. —Sir William Bagge, Bart., M.P., Stradsett Hall, Market
Downham, Norfolk; Colonel James Theslie Tait, Montgomery,
Alabama, U.S.; and Dr. A. A. Caruana, The University, Malta.
25th.—George Cox Bompas, Esq., 15 Stanley Gardens, Ken-
sington Park, W.; Sir James Anderson, 16 Warrington Crescent,
W.; and John Breedon Everard, Esq., 6 Millstone Lane, Leicester.
June 8th.—Henry G. Vennor, Esq., Geological Survey of Canada,
Montreal; Alexander Kendall ilfvaanagra, Esq., Director-General
of Public Wiens Montevideo, South America ; and Arthur Roope
Hunt, Esq., Quintella, Torquay.
22nd .—Horace Pearce, Hsq., 21 Hogley Road, Stourbridge ;
and Samuel Spruce, Esq., Tamworth.
November 9th.—Lieut. Reginald Clare Hart, R.E., Brompton Bar-
racks, Chatham; Lieut. James F. Lewis, R.E., Brompton Bar-
racks, Chatham; and M. F. Maury, Jun., Ksq., 1300 Main Street,
Richmond, Virginia, U.S.
December 7th.—Rey. J. W, Todd, D.D., Tudor House, Sydenham,
_ ANNUAL REPORT, vil
. S.H.; Hon, Henry Ayers, Adelaide, South Australia; R. W. Pere-
grine Birch, Esq., Palace Chambers, Westminster, S.W. ; Alfred
_ Stair, Esq., 4 Surinam Terrace, Stratford, Essex; Harry Rivett
Carnac, Esq., Simla, Kast Indies; Thomas Davies, Esq., British
. Museum, W.C., and 47 Rutland Road, South Hackney, E.;
Rey. J. H. Cooke, Northbourne Rectory, Deal; J. 8. Courtney,
| Esq., Penzance ; John Johnson, Hsq., Chilton Hall, Ferry Hill,
Durham ; Rey. R. H. Morris, M.A., Training College, Carmarthen ;
and Joseph Drew, Esq., Belgrave Terrace, Weymouth.
December 21st.—Valentine D. Colchester, Esq., 4 Buckland Villas,
Belsize Park, N.W.; H.J.Heighton, Esq., Gold Street, Kettering ;
Thomas Hawksley, Esq., 30 Great George Street, 8.W.; Frank
_ Rutley, Esq., Geological Survey of England, Museum, J ermyn
' Street, S.W.; and Isaac Roberts, Esq., 26 Rock Park, Rockferry,
Cheshire.
The following Donations to the Musrum have been received since
the last Anniversary Meeting.
Specimens of Hophyton and other Cambrian fossils; presented by
Professor Otto Torell, F.C.G.S.
Electrotype casts of Asaphus platycephalus showing limbs ; presented.
_by E. Billings, Esq., F.G.8., and Sir W. E. Logan, F.R.S., F.G.S.
Corals from the South-Australian Tertiaries ; presented by Prof. P.
Martin Duncan, M.B., F.R.S., F.G.S.
Fossils from the Suffolk Tertiaries; presented by EH. Ray Lankester,
Hsq., B.A.
Rock specimens from Tideswell Dale; presented by the Rev. J. M.
Mello, F.G.S.
Models of South-African Diamonds; presented by Prof. Tennant,
F.G.S.
Model of the head of a large ee presented by G. Maw,
Esq., F.G,8, ;
ee CHARTS, ETC. PRESENTED.
Geological Map of Queensland: Cape-Riyer Gold-field (2 sheets) and.
Canal-Creek Digeings; presented by the Geological Survey of
Queensland. .
Geological Survey Map of Sweden, Sheets 31-35, with 5 parts of
descriptions and Geological Map of Ostradal ; presented by the
Director of the Swedish Geological Survey, Prof, A. Erdmann.
Geological Survey Map of Prussia and the Thuringian States, Sheets
237-239 and 255-257, with explanations and introductory re-
marks ; presented by the Prussian Minister of Commerce and
Public Works.
Geological Survey Map of Austria, Sheets 1 and 2, with explana-
tions; presented by the Director of the Austrian Geological Survey,
Franz Ritter von Hauer, F.C.G.S. _
Geological Survey Map of Switzerland, Sheets 6, 7, and 22, with a
sheet of Sections; presented by the Swiss Geological Commission.
viii ANNIVERSARY MEBTING.
Map of Lundy Island, Geologically coloured and presented by N.
Whitley, Esq.
Lithological Map of the Embouchure of the Seine, by M. E. Bese :
presented by the Author.
Sketch-Map of the Geology of New Zealand, by Dr. James Hector,
FE.RS., F.G.8.; presented by the Author.
Geological Map of Wisconsin, by F. A. Lapham, Esq.; presented by
_ the Author.
The following Lists contain the Names of Persons and Public
Bodies from whom the Society has received Donations to the Library
and Museum since the last Anniversary Meeting, February 18, 1870.
I. List of Societies and Public Bodies from whom Donations of Books
have been received since the last Anniversary Meeting
Bath, Natural-History and An-
Devonshire Scientific _ Associa-
tiquarian Field-Club of.
Belfast. Naturalists’ Field-Club.
Berlin. German Geological So-
ciety.
, Society of Naturalists at.
. Royal Prussian Academy.
Berwick. Berwickshire Natu-
ralists’ Field-Club.
Birmingham Free Library, Com-
mittee of.
Bordeaux, Linnean Society of.
Boston, Society of Natural His-
tory of..
Brussels. Royal Academy of
Belgium.
Calcutta. Asiatic Society of
Bengal.
Cambridge (Mass.). American
Association for the Advance-
ment of Science.
American Academy of
Arts and Sciences.
Canadian Institute.
Copenhagen. Royal Danish Aca-
demy.
Cornwall, Royal Geological So-
ciety of.
Darmstadt. Geological Society
of the Middle Rhine.
tion.
Dorpat, Natural-History Society
f.
of.
Dresden, (Isis) Natural-History
Society of.
Dublin. Royal Dublin Society.
Royal Geological Society
of Ireland.
Royal Irish Academy. .
Kast-India Association.
Edinburgh, Geological Society of.
, Royal Physical Society of.
——, Royal Society of.
Florence. Royal Geological
Committee of Italy.
Frankfort. Senckenbergian Na-
tural-History Society.
Glasgow, Geological Society of.
Gloucester. Cotteswold Natu-
ralists’ Field-Club.
Haarlem, Society of Sciences of.
Halifax (N.8.). Nova-Scotian
Institute of Natural Science.
Halle, Natural-History Soe. of.
Heidelber g, Natural-History and
Medical Society of.
Indian Government.
ANNUAL REPORT. ix
Lausanne. . Vaudoise Society of
Natural Sciences.
Leeds, Literary and Philosophical
Society of. .
Liverpool, Geological Society of.
Historic Society of Lan-
cashire and Cheshire.
London, Art Union of.
British Association.
Chemical Society.
Geologists’ Association.
Institution of Civil En-
gincers.
Linnean Society.
—. London Institution.
Paleontographical © So-
——-—
e
—
.
ciety.
. Photographic Society.
Quekett Microscopical
Club.
Royal Agricultural So-
ciety of England.
Royal Asiatic Society of
Great Britain.
Royal Astronomical So-
ciety.
Royal College of Sur-
geons.
Royal Geographical So-
ciety.
Royal Institution.
——. Royal Society.
—. Society of Arts.
— , Zoological Society of.
Maine, Commissioners of Fish-
eries of the State of.
Melbourne. Geological Survey
of Victoria.
Mining Survey of Vic-
toria.
Milan. Italian Society of Natural
Sciences.
Minnesota, Government of.
Moscow, Imperial Society of
Naturalists of.
Munich, Academy of Sciences of.
Neuchatel, Society of Natural
Sciences of.
Neweastle-on-Tyne. Natural-
History Society of Northum-
berland and Durham.
Iron ,and Steel Insti-
tute.
North of England Insti-
tute of Mining Engineers.
New York, American Museum of
Natural History of.
, Lyceum of Natural History
of.
, Regents of the University
of.
——, State Cabinet of.
New Zealand, Geological Survey
of.
, Government of.
—— Institution.
Offenbach, Natural-History So-
ciety of.
Paris. Academy of Sciences.
Dépot de la Marine.
Geological Society of
France.
Philadelphia, Academy of Natural
Sciences of.
American Philosophical
Society.
Plymouth Institution.
Puy. Society of Agriculture,
Arts, &¢.
Queensland, Geological Survey of.
Salem. Peabody Academy of
Sciences.
Essex Institute.
St. Petersburg, Academy of
Sciences of.
Strasbourg, Society of Natural
Sciences of. -
Stuttgart. Natural-History So-
ciety of Wiirttemberg.
Swiss Geological Commission.
Switzerland, Natural - History
Society of.
Sydney. Royal Society of New
South Wales.
x ANNIVERSARY MEETING.
2
Teignmouth., Teign Naturalists’
_ Field-Club.
ee Royal ay of Sciences
Mote
United States Government. :
, Patent Office of,
Vienna, Imperial Academy of
Sciences of.
, Geological Institute of,
Victoria, Government of.
Warwickshire Naturalists’ Field-
Club.
- Wiesbaden. ©
- Washington.
Natural - History
Society of Nassau.
Smithsonian In-
stitution.
Wolverhampton, South Midland
Institute of Mining, Civil, and
Mechanical Engineers,
York. Yorkshire Philosophical
Society.
Yorkshire, Geological and Poly-
technic Society of the West.
Riding of,
—— Naturalists’ Club,
II. List containing the names of Persons from whom Donations to
the Library and Museum have been received since ihe last
Anniversary Meeting.
Abich; Dr. H., F.M.G.S,
Academy, Editors of the.
Achiardi, Sig, A. d’.
Adams, Dr. A. Leith, F.G.S
Agassiz, Prof. L., F. M. G. Sy
Agriculture, Tatiadl States eh tie,
missioners of.
American Journal of Conchology,
Editor of the.
American’ Journal of Science,
Editors of the.
Anderson, B., Esq.
Annales des Mines, Editors of
the.
Ansted, Prof. D. T., F.G.8,
Archer, W. H., Esq.
Athenssum, Editor of the.
Barrande, M. J., F.M.G.S.
Bauerman, H., Esq. pt GS,
Beckles, 8. H., Esq., F.G.8,
Belerand, M. h,
Bell, A. , Esq.
Billings, E., Esq., F.G.S.
Binney, ‘B, W., Esq., F.G.S.
Binney, W. D., Esq.
Bonney, Rey. T. G., F.G.S.
Bowerbank, Dr. J. S., HGS.
Brandt, Dr, F., F.C. GS.
Brodie, Rey. P. Bop HGady
Broome, G., Esq., F,G.S._
Brown, BR. E. , Esq., F.G.S..
Canadian J ournal, Lditors of
_ the.
Carpenter, Dr. W. B., F.G.S,
Cartailhac, M.
Caruana, Dr. A. A., F.G.S,
Catlin, G., Ksq.
Ceselli, Sic.
Ghemicnl News; Editor of the,
Christy, H., Esq., Executors of
the late,
Colliery Guardian, Editor of the.
Cook, Prof. G. H.
Cornalia, Dr. E.
Croll, J., Esq.
Dall, W. H., Esq.
Daubrée, M., F.M.G.S.
Davidson, T., Esq., F.G.S,
Dawson, Prof, J. W., F.G.S,
Desguin, M. P.
Deslongchamps, M. Eugene.
Dewalque, M. G.
Duncan, Prof. P. Martin, F.G.S.
Eichwald, Dr. E. von.
Electric Telegraph and Railway
Review, Editor of the.
ANNUAL REPORT, xl
English Mechanic, Hditor of the.
Evans, Caleb, Esq., F.G.S.
Evans, J ohn, Esq., F.G.8.
Fayre, M. A., F.C.G.S.
Foetterle, Dr. F.
Fuchs, M. T.
Geinitz, Dr., F.M.G.S.
Geological Magazine, Editors of
the.
Gilliéron, M. V.
Giimbel, Dr., F.C.G.S,
Haidinger, Prof. W. von,
F.M.G.S.
Hall, Dr. James, F.M.G.S.
Hall, Marshall, Esq., F.G.S.
Hamilton, Mrs. W. J.
Hartley, E., Hisq., F.G.S.
Hasskarl, Dr. C.
Hayden, E. V., Esq.
Hébert, M. E., F.C.G.S.
leant, Dr. J acne, ENGESe
Helmersen, Gen. G. von,
F.M.G.S8.
Hill, J., Esq.
Hoffmann, Dr. C.
Hopkinson, John, Hsq., F'.G.8.
Hull, H. M., Esq.
Hunt, Dr. T. Sterry.
Iron and Coal Trades Review,
~ Editors of the.
Jeffreys, J. Gwyn, Esq., F.G.S.
Jahrbuch fiir Mineralogie, Geo-
logie, &c., Editors of the.
Jones, Prof. T. Rupert, F.G.8.
Karrer, Dr. F.
Kayser, M. E.
Kawall, M. J. H.
King, Prof. W.
Lankester, HE. Ray, Esq.
Lapham, F. A., Hsq.
Lea, Isaac, Esq.
Linnarsson, M. J. G. O.
Logan, Sir W. E., F.G.S.
London, Edinburgh, and Dublin
Philosophical Magazine, Edi-
tors of the.
Longman & Co,, Messrs,
Lorenz, M. L.
Lubbock, Sir J., Bart., F.G.8.
Lyell, Sir Charles, Bart. F.G.8,
Mackintosh, D., Esq., F.G.S.
Marcou, M. Jules.
Marsh, Prof. C. O., F.G.8.
Maw, G., Esq., ¥.G.S.
Maw, H. L., Esq.
Mayer, M. K.
Mello, Rev. J. M., F.G,S,
Mojsisovics, M. HK. von.
Montagna, Sig. C.
Monthly Microscopical J ournal,
Editors of the. .
Moore, Charles, Esq., F.G.S
Morris, Prof. John, Tr. G.S.
Murchison, Sir R. Jet Bart?
IGS),
' Naturalists’ Note Book, Editor
OP olthe:
Nature, Editor of.
Newberry, Dr. J.8.
Nova Scotia, Chief Commissioner
of Mines of.
Nyst, Digi E0638.
Oustalet, M.
Packard, Dr. A. 8., Jun.
Parfitt, H., Hsq.
Parrish, R. A., Jun., Esq.
Pascucci, Prof. L. D:
Pearce, H., Esq., F.G.S,
Perry, J. B., Esq.
Pessina, Sig. L. J.
Piggot, J., Jun., Hsq., F.G.8.
Prestwich, Jos., Esq., F.G.8.
Quarterly Journal of Science,
Editors of the,
Quetelet, M. A.
Ramsay, Prof. A. C., F.G.8.
Raynolds, Gen. W. F.
Reuss, Prof. A. E., F.C.G.8.
Revue des Cours Scientifiques,
Kditors of the.
xii ANNIVERSARY MEETING.
Richards, Admiral, R.N.
Richthofen, Baron F. von.
Rickard, Major F. J., F.G.S8.
Rowney, T. H., Esq.
Safford, J. N., Esq.
Sandberger, Prof. F., F.C.G.S.
Sauvage, M.
Schloenbach, Dr. U.
Scientific Opinion, Editors of.
Seeley, H.-G., Esq., F.G.8.
Sorge, Dr. C. T.
Spratt, Capt. T. A. B., F.G.S.
Steen, M. Adolph.
Streeter, G. L., Esq.
Student and Intellectual Observer,
Kditors of the.
Studer, Prof. B., F.M.G.8.
Suringar, Dr. W. F. R.
Tate, R., Esq., F.G.8.
Tennant, Prof. J., F.G.S.
Thomsen, Prof. J.
Thomson, Prof. Wyville, F.G.S.
Torell, Prof. Otto, F.C.G.S.
Trautschold, M. H.
Trutat, M.
Turin, Director of the Observa-
tory of.
Ulrich, G. H. F., Esq., F.G.S.
Ungarische Revue, Editor of the.
Walther, Dr. C. F.
Watson, R.8., Esq.
Weyenbergh, Dr. H.
Whitaker, W., Esq., F.G.8.
Whittlesey, C. E., Esq.
Winkler, Dr. T. C.
Woodward, H. B., Esq., F.G.8.
Wright, Dr. T., F:G:8:
Wynne, A. B., Esq., F.GS.
Zeuschner, Prof. L.
Zigno, Baron A. de, F.C.G.S.
Zirkel, Prof. F., F.C.G.8.
Zittel, Dr. K. A.
Last of Parurs read since the last Anniversary Meeting,
February 18th, 1870.
1870.
February 23rd.—Additional Observations on the Neocomian Strata
in Yorkshire and Lincolnshire, with Notes on their Relations to
the Beds of the same age throughout Northern Europe, by
J. W. Judd, Hsq., F.G.8.
On Deep-mining with Relation to the Physical Struc-
ture and Mineral-bearing Strata of the South-west of Ireland, by
Samuel Hyde, Esq.; communicated by R. Etheridge, Ksq.,
F.G.S.
March 9th.—On the Structure of a Fern-stem from the Lower
Eocene of Herne Bay, and on its Allies, Recent and Fossil, by
W. Carruthers, Esq., F.L.S., F.G.S.
On the Oolites of Northamptonshire, by Samuel Sharp,
Esq., F.G.8.
March 23rd.—Notes on a Skull from the Upper Cretaceous of Griin-
bach, by Dr. Emanuel Bunzel ; communicated by Prof. Huxley,
IN Gasby JOA Case
On the Discovery of Organic Remains in the Caribbean
Series of Trinidad, by R. J. Lechmere Guppy, Hsq., F.LS.,
F.G.8.
——~-—— On the Paleontology of the Junction Beds of the Lower
ANNUAL REPORT, xili
and Middle Lias in Gloucestershire, by Ralph Tate, Esq., A.L.S.,
March 23rd.—Geological Observations on the Waipara River, New
Zealand, by T. H. Cockburn Hood, Esq., F.G.S.
On the Fall of an Aerolite in Fezzan, by M. Coum-
bary ; communicated by R. H. Scott, Esq., F.G.S.
April 13th.—On Australian Fossil Mammals, by Dr. Gerard Krefft ;
communicated by H. M. Jenkins, Esq., F.G.8.
On Fossil Remains of Mammals found in China, by Prof.
Owen, LL.D., F.R.S., F.G.S.
. Further Discovery of the Fossil Elephants of Malta, by
Dr. A. A. Caruana; communicated by Dr. A. Leith Adams,
F.G.S.
April 27th.—On the Species of Rhinoceros whose Remains were
discovered in a Fissure-cavern at Oreston in 1816, by G. Busk,
Ksq., F.R.S., F.G.S.
On two Gneissoid Series in Nova Scotia and New Bruns-
wick, supposed to be the equivalents of the Huronian (Cambrian)
and Laurentian, by H. Youle Hind, Esq., M.A.; communicated
by Prof. Ramsay, F.R.S., F.G.S.
May 11th.—Notes on some ’ Specimens of Lower-Silurian Trilobites,
by E. Billings, Esq., F.G.S.
Note on the Palpus and other Koneudstes of Asaphus
from the Trenton Limestone, in the British Museum, by H. Wood-
ward, Esq., F.G.8.
On the Structure and Affinities of Sigillaria, Calamites,
and Calamodendron, by J. W. Dawson, LL.D., F.R.S., F.G.S.
Notes on the Geology of Arisaig, Nova Scotia, by the
Rey. D. Honeyman, D.C.L., F.G.8.
May 25th.—Contributions to a Knowledge of the Newer Tertiaries
of Suffolk and their Fauna, by E. Ray Lankester, Esq. ,B.A. ;
communicated by Prof. Huxley, F.R.8., F.G.S.
———— Notes on an Ancient Boulder-clay of Natal, by Dr.
Sutherland ; communicated by Prof. Ramsay, F.R.S., F.G.8.
— On the Distribution of Wastdale-Crag Blocks, “ Shap-Fell
Granite Boulders,” in Westmoreland, by Professor Robert Hark-
ness, F'.R.S., F.G.8.
June 8th.—On the Superficial Deposits of the South of Hampshire
and the Isle of Wight, by Thomas Codrington, Esq., F.G.S.
: On the Relative Position of the Forest-bed and the
Chillesford Clay in Norfolk and Suffolk, and on the Real Position
of the Forest-bed, by the Rey. John Gunn, M.A., F.G.S.
On a new Labyrinthodont Amphibian from the Magnesian
Limestone of Midderidge, Durham, by Albany Hancock, Esq.,
F.L.S., and Richard Howse, Esq.; communicated by Prof.
Huxley, F.R.S., F.G.S.
On Proterosawrus Spenert, Von Meyer, and a new species,
Proterosaurus Huxleyi, from the Marl-slate of Midderidge, Dur-
ham, by Albany Hancock, Esq., F.L.S., and Richard Howse, Esq.;
communicated by Prof. Huxley, F.R.S., F.G.8.
xiv: ANNIVERSARY MEETING.
June 22nd.—Notes on the Lower Portion of the Green Slates and
Porphyries of the Lake-district between Ulleswater and Keswick,
- by H. A. Nicholson, M.D., D.Sc., M.A., F.G.S.
Observations on Sonn Veoetable Fossils from Victoria,
. by Dr, Ferd. yon Miller, and R. Brough Smyth, Esq., F.G.8.
Note.on some Plesiosaurian Remains obtained by J. C.
- Mansel, Esq., F'.G.8., in Kimmeridge Bay, Dorset, by J. W.
Hulke, Esq., F.R.S., F.G.S.
Notes on the Geology of the Lofoten Islands, by the Rey.
es Bonney, M.A., E.G.S.
On Dorypterus Hoffmanni, Germar, from the Marl-slate of.
Midderidge, Durham, by Albany Hamcods Ksq., -F.L.8., and
Richard Howse, Esq.; communicated by Prof. Huxley, E.R.S., E.G. 8.
Observations on Ice-marks in Newfoundland, by Staff-
; Comm. J. H. Kerr, R.N.; communicated by Sir. R. I. Murchison,
Bart., F.R.S., F. GS.
——— On the Glacial Phenomena of Western Lancashire and
Cheshire, by C. E. De Rance, Esq., F.G.S.
———- On the Postglacial Deposits of Western Lancashire and
Cheshire, by C. E. ne Rance, Esq., F.G.8.
Observations on Modern Glacial Action in Canada, by
the Rev. W. Bleasdell, M.A.; communicated by Principal Daw-
- son, F.RB.S., F.G.S8.
— On an Altered Clay-bed and Sections in Tideswell Dale,
| Derbyshire, by the Rev. J. M. Mello, M.A., F.G.8.
On the Physics of Arctic Ice as Explanatory of the
" Glacial Remains in Scotland, by Dr. Robert Brown, M.A.; com-
; Municated by Prof. Ramsay, ER. S., F.G.8.
November 9thi—On the Carboniferous Flora of Bear Island (lat.
74° 30! N.), by Prof. Oswald Heer, F.M.G.S.
On the Evidence afforded by the Detrital Beds with-
out and within the North-eastern part of the Valley of the Weald
_as to the Mode ‘and Date of the Denudation of that Valley, by
Searles V. Wood, jun., Esq., F.G.S.
November 23rd.—On some Points in South-African Geology, Part I.,~
_ by G. W. Stow, Hsq.; communicated by Prof. T. Rupert Jones,
el
Note on some Reptilian Fossils from Gozo, by J. W.
Hulke, Esq., F.R.S., F.G.8.
On the Discovery of a “ Bone- bed ” in the lowest of
the “ Lynton Grey Beds,” North Devon, by F. Royston Fairbank,
M.D. ; communicated by Prof. Duncan, M.B., F.R.S., Sec. G.S.
December 7th.—On Fossils from Cradock and elsewhere in South
Africa, by George Grey, M.D. ; communicated by Prof. T. Rupert
Jones, F.G.8.
On some points in South-African Geology, Part IT.,
by G. W. Stow, Esq.; communicated by Prof. T. Rupert Jones,
E.G.S.
On the Geology of Natal, in South Africa, by C. L.
Griesbach, Esq. ; communicated by H. "Woodward, Esq., F.G.S.
ANNUAL REPORT, ~ “XV
December 7th.—On the Diamond-districts of the Cape of Good
Hope, by G. Gilfillan, Esq.; communicated by Warington Me
Smyth, Esq., F.R.S., EGS.
December 21st.—On Lower Tertiary Deposits recently exposed. at
Portsmouth, by C. J. A. Meyer, Esq., F.G.S.
Note on some New Crustacea from the Lower
Kocene of Portsmouth, collected by C. J..A. Meyer, Esq., F.G.S.,
by H. Woodward, Esq., F.G.8.
On the Chalk of the Cliffs from Seaford to Eastbourne,
Sussex, by W. Whitaker, Esq., B.A., F.G.S.
— On the Chalk of the Southern part of Dorset and
Devon, by W. Whitaker, Esq., B.A., F.G.S.
1871. ie
January 11th.—On the older Metamorphic Rocks and Granite of
Banffshire, by T. F. Jamieson, Esq., F.G.S.
— On the Connexion of Volcanic Action with Changes
of Level, by Joseph John Murphy, Esq., F.G.S.
On some points in the Geolog gy of the Neighbourhood
of Malaga, by Don M. de Orueba; communicated by Sir R. I.
Murchison, Bart., F.R.S., F.G.S. °
January 25th.—On the Physical Relations of the New Red Marl,
Rheetic Beds, and Lower Lias, by Prof. A. C. Ramsay, LL.D.,F.R.S.,
F.G.8.
Note on a large Reptilian Skull from Brooke, Isle
of Wight, probably Dinosaurian, and referable to the Genus
Iguanodon, by J. W. Hulke, Hsq., F.R.S., E.G.S.
February 8th.—On the Punfield Formnanon, by J. W. Judd, Esq.,
F.G.S.
Some Remarks on the Denudation of the Oolites of
the Bath District, with a Theory on the Denudation of Oolites
generally, by W. 8. Mitchell, Esq., LL.B., 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.
he
It was afterwards resolved,—
That the .thanks of the Society be given to R. A. C. Godwin-
Austen, Esq., and to Warington W. Smyth, Esq., retiring from the
office of Vice-President.
That the thanks of the Society be given to Professor Duncan,
retiring from the office of Secretary. ;
That the thanks of the Society be given to Harvey B. Holl, M.D.,
G. Maw, Esq., J. C. Moore, Esq., Warington W. Smyth, Esq., and the.
Rev. W.S. Symonds, M.A., retiring from the Council.
XVi
ANNIVERSARY MEETING.
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.
Joseph Prestwich, Esq., F.R.S.
VICE-PRESIDENTS.
Sir P. de M. G. Egerton, Bart., M.P., F.R.S.
Prof. T. H. Huxley, LL.D., F.R.S.
Sir Charles Lyell, Bart., D.C.L., F.R.S.
Prof. John Morris.
SECRETARIES.
John Evans, Esq., F.R.S., F.S.A.
David Forbes, Esq., F.R.S.
OREIGN SECRETARY.
Prof. D. T. Ansted, M.A., F.R.S.
TREASURER.
J. Gwyn Jeffreys, Esq., F.R.S,
——
COUNCIL.
Prof. D. T. Ansted, M.A., F.R.S.| J. Whitaker Hulke, Esq., F.R.S.
W. B. Carpenter, M.D., F.R.S. | Prof.T. H. Huxley, LL.D., F.R.S. |
William Carruthers, Esq., F.L.S.| J. Gwyn Jeffreys, Esq., F.R.S.
W. Boyd Dawkins, Esq., M.A.,| Sir Charles Lyell, Bart., D.C.L»
F.R.S
E.R.S.
Prof, P. Martin Duncan, M.B.,| C. J. A. Meyer, Esq.
F.R.S. Prof. John Morris.
Sir P. de M. G. Egerton, Bart., | Joseph Prestwich, Esq., F.R.S.
M.P., F.R.S. Prof. A.C. Ramsay, LL.D.,F.R.S.
John Evans, Esq., F.R.S., F.S.A.| R. H. Scott, Esq., M.A., F.R.S.
David Forbes, Esq., F.R.S. Prof. J. Tennant.
J. Wickham Flower, Esq. Rev. Thomas Wiltshire, M.A.,
Capt. Douglas Galton, C.B., F.BR.S. BRAS.
R, A. C. Godwin-Austen, Hsq.,| Henry Woodward, Esq.
XVii
LIST OF
THE FOREIGN MEMBERS
OF THE GEOLOGICAL SOCIETY OF LONDON, 1 1870.
Date of
Election.
1819. Count A. Breunner, Vienna.
1822. Count Vitaliano Borromeo, Milan.
1827. Dr. H. von Dechen, Bonn.
1828. M. Léonce Elie de Beaumont, Sec. Perpétuel de 1’Instit. France
For. Mem. R.S., Paris.
1829. Dr. Ami Boué, Vienna.
1829. Dr. J. J. d’Omalius d’Halloy, Halloy, Belgium.
1839. Dr. Ch. G. Ehrenberg, For. Mem. R.S., Berlin.
1840. Professor Adolphe T. Brongniart, For. Mem. R.S., Parvs.
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.
1848. James Hall, Esq., Albany, State of New York.
1850. Professor Bernard Studer, Berne.
1851. Professor James D. Dana, New Haven, Connecticut.
1851. General G. von Helmersen, S¢. Petersburg.
1851. Dr. W. K. von Haidinger, For. Mem. R.S., Vienna.
1851. Professor Angelo Sismonda, Twrin.
1853. Count Alexander von Keyserling, Dorpat.
1855. Professor L.G. de Koninck, Liége.
1854, M. Joachim Barrande, Prague.
1854. Professor Carl Friedrich Naumann, Lezpsic.
1856. Professor Robert W. Bunsen, For. Mem. R.S., Hezdelberg.
1857. Professor H. R. Goeppert, Breslau.
1857. M. E. Lartet, Paris.
1857. Professor H. B. Geinitz, Dresden.
1857. Dr. Hermann Abich, Tiflis, Georgia.
1858. Herr Arn. Escher von der Linth, Zurich.
1859. Professor A. Delesse, Paris.
1859. Dr. Ferdinand Roemer, Breslau.
1860. Dr. H. Milne-Edwards, For. Mem. R.8., Paris.
1862. Baron Sartorius von Waltershausen, Gottingen.
1862. Professor Pierre Merian, Basle.
1864. Professor Paolo Savi, Pisa.
F YOu, xxv. b
soni
1865. M. Jules Desnoyers, Pars.
1866. Dr. Joseph Leidy, Philadelphia.
1867. Professor A. Daubrée, Paris.
1870. Professor Oswald Heer, Zurich.
LIST OF
THE FOREIGN CORRESPONDENTS
OF THE GEOLOGICAL SOCIETY OF LONDON, in 1870,
Date of
Election.
1863. Professor E. Beyrich, Berlin.
1863. Herr Bergmeister Credner, Gotha.
1863. M. E. Desor, Neuchatel.
1863. Professor Alphonse Favre, Geneva,
1863. Signor B. Gastaldi, Zea.
1863. M. Paul Gervais, Montpellier.
1863. Herr Bergrath Gumbel, Munich.
1863. Dy. Franz Ritter von Hauer, Vienna.
1863. Professor E. Hébert, The Sorbonne, Paris.
1863. Dr. G. F. Jager, Stuttgart.
1863. Dr. Kaup, Darmstadt.
1863. M. Nikolai von Kokscharow, St. Petersburg.
1863. M. Lovén, Stockholm.
1863. Count A. G. Marschall, Vienna.
1865. Professor G. Meneghini, Pisa,
1863. M. Henri Nyst, Brussels.
1863. Professor F. J. Pictet, Geneva.
1863. Signor Ponzi, Rome.
1863. Professor Quenstedt, Tiibingen.
1863. Professor F. Sandberger, Bavaria.
1863. Signor Q. Sella, Turin.
1863. Dr. F. Senft, Hisenach.
1863. Professor E. Suess, Vienna.
1863. Marquis de Vibraye, Paris,
1864. M. J. Bosquet, Maestricht.
1864, Dr. Theodor Kjerulf, Christiania.
1864. Dr. Steenstrup, Copenhagen.
1864. Dr. Charles Martins, Montpellier.
1865. Dr. C. Nilsson, Lund.
1866. Professor J. P. Lesley, Philadelphia.
1866. M. Victor Raulin, Paris.
1866. Professor August Emil Reuss, Vienna.
1866.
1867.
1868.
1869.
1869.
1869.
1870.
1870.
“cc To
XxX
Baron Achille de Zigno, Padua.
Professor Bernhard Cotta, Freiburg.
M. Albert Gaudry, Paris.
Professor J. F. Brandt, St. Petersburg.
Professor A. E. Nordenskiéld, Stockholm.
Professor F. Zirkel, 38 Frankfurter Strasse, Leipzig.
Professor Joseph Szabo, Pesth.
Professor Otto Torell, Lund.
AWARDS OF THE WOLLASTON MEDAL
UNDER THE CONDITIONS OF THE “DONATION FUND”
ESTABLISHED BY
WILLIAM HYDE WOLLASTON, M_D., F-RS., F.GS8., &.
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.
1835.
1836.
1837,
1838.
Mr. William Smith. 1854. Dr. Richard Griffith.
Dr. G. A. Mantell. 1855. Sir H. T. De la Beche.
M. L. Agassiz. 1856. Sir W. E. Logan.
ee P. T. Cautley. 1857. M. Joachim Barrande.
Dr. H. Falconer. 1858. ee Hermann von Meyer.
Professor R. Owen. Mr. James Hall.
1839. Professor C. G. Ehrenberg. 1859. Mr. Charles Darwin.
1840. Professor A. H. Dumont. 1860. Mr. Searles V. Wood.
1841. M. Adolph T. Brongniart. 1861. Professor Dr. H. G. Bronn.
1842. Baron L. von Buch. 1862. Mr. Robert A. C. Godwin-
1843. i E. de Beaumont. Austen.
M. P. A. Dufrénoy. 1863. Professor Gustav Bischof.
1844. The Rev. W. D. Conybeare, | 1864. Sir R. I. Murchison.
1845. Professor John Phillips. 1865. Mr. Thomas Davidson.
1846. Mr. William Lonsdale. 1866. Sir Charles Lyell.
1847. Dr. Ami Boué. 1867. Mr. G. P. Scrope.
1848. The Rev. Dr. W. Buckland. | 1868. Professor Carl F. Naumann.
1849. Mr. Joseph Prestwich. 1869, Mr. H. C. Sorby.
1850. Mr. William Hopkins. 1870. Professor G. P. Deshayes.
1851. The Rey. Prof. A. Sedgwick. | 1871. Professor A. C. Ramsay.
1852.
1853
Dr. W. H. Fitton.
M. le Vicomte A. d’Archiac.
* |M. E. de Verneuil.
xx
AWARDS
OF THI
BALANCE OF THE PROCEEDS OF THE WOLLASTON
“ DONATION-FUND.”
1831.
1833.
1854.
1835.
1836.
1838.
1839.
1840,
1841.
1842.
1843.
1844.
1845.
1846.
1847.
1848.
1849.
1850.
1851.
1852.
Mr. William Smith.
Mr. William Lonsdale.
M. Louis Agassiz.
Dr. G. A. Mantell.
M. G. P. Deshayes.
Professor Richard Owen.
Professor C. G. Ehrenberg.
Mr. J. De Carle Sowerby.
Professor Edward Forbes.
Professor John Morris.
Professor John Morris.
Mr. William Lonsdale.
Mr. Geddes Bain.
Mr. William Lonsdale.
M. Alcide d’Orbigny.
M. Alcide d’Orbigny.
Mr. William Lonsdale.
Professor John Morris.
M. Joachim Barrande.
Professor John Morris.
Cape of Good Hope Fossils.
1855.
1854,
1855.
1856.
1857.
1858.
1859.
1860.
1861.
1862.
1865.
1864.
1865.
1866.
1867.
1868.
1869.
1870.
1871.
M. L. de Koninck.
Mr. 8. P. Woodward.
Drs. G. and F. Sandberger.
M. G. P. Deshayes.
Mr. 8S. P. Woodward.
Mr. James Hall.
Mr. Charles Peach.
Mr. T. Rupert Jones.
be W. K. Parker.
Professor A. Daubrée.
Professor Oswald Heer.
Professor Ferdinand Senft.
Professor G. P. Deshayes.
Mr. J. W. Salter.
Mr. Henry Woodward.
Mr. W. H. Baily.
M. J. Bosquet.
Mr. W. Carruthers.
M. Marie Rouault.
Mr. R. Etheridge.
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Xxil
EstiMaTEs for
INCOME EXPECTED.
Due for Subscriptions for Quarterly Journal (con-
SId CrediGOOd)eariemcicelselieetescieriseecelieeiteeeeistes 13 0 0
Due for Authors’ Corrections — ...........sseeseeees 20 0 O
Due for Arrears (See Valuation-sheet) ..........0« 234 10 6
— 26710 6
Estimated Ordinary Income for 1871.
Annual Contributions :—
From Resident Fellows, and Non-residents
CON e TUSVEXD) CO AMEXOI Goaaasacsocoaobocdoocqucauodagcec Vessssosees SOOM OO
Admission-fees (supposed) ...... Soganonedaspoedeh cone series (2 DOO
Compositions (Supposed) 2.0.2. ..0ccc-cacoceraceresecsccasens 250 O
Dividends on@onsols)) vc2scc...nsscsesecescece wdsfeseuuamenese sen 163 9 10
Sale of Transactions, Proceedings, Library-cata-
logues, Ormerod’s Index, and Hochstetter’s New
Zealand ......+6 desleva vacates re Hee aaon ea ggenncswenos 15 0 O
Sale of Quarterly Journal ...... Sede deel ssiecewesietee 150 O
Sale of Geological Map ............ Wedouidoce= ees td ae 2D
— 190 0 0
Due from Longman and Co. in June............... 54 8 1
Due from Stanford and Co. in June ......... 930000 13 4 8
ce 67 12 9
£2038 13 1
J. GWYN JEFFREYS, Treas.
Feb. 6, 1871.
» XXii
the Year 1871.
EXPENDITURE ESTIMATED.
£ s. d. aes
General Expenditure :
Taxes and Insurance..............- ceeeeee 40 0 0
INNIER® Sooo ocd doco oecKdgsodeNDGOONRE 1 0 0
House-repairs soddeapoe000g00e 30 0 0
Intell oseddonccoscndosodoo 00 opoando0 D000 30 0 0
Light +0... BRAM UOTE Sb soak ris bids 30 0 0
Miscellaneous House-expenses .........-... 65 0 0
SiQGOMORY ao ob pQo0 Gd oGDO BN oaOOS AAI AOAn 25 0 0
Miscellaneous Printing, including Abstracts -. 75 0 0
Tea for MeetingS ....-0..cccsceccceccsees 25 0 0
335 O
Salaries and Wages:
Assistant Secretary ........cccececcesvece 300 0 0
Clerkg eee esas sogcdcaoCou SO doCdC0dS 120 0 0
Assistant in Library and Museum -se- 65 0 O
POP scooocdpoancoc: gd do gobo Aba ane -- 100 0 0
ELQUSed ald ieeaveletelerclonslelaelelierelsierloleieictelereier 40 0 0
Occasional Attendants .........0..-e00.00 10 0 0
Wollectoneertetcttetsicelesoiettenseitisraier= gn oned 20 0 0
ANGELINA Senn 6 aplsoooodo Dongddbe. Tor 5 0 0
660 0O
ADGA Arte cseeeel leet docmsas sionals os Sopoocsosoneadsocget0 100 0 O
MINS CUM eeroe ccaniataranee secac erase seiseuiceemamcecmcaa Gros 5 0. 0
——— 105 0
Wis cellaneons IX PCNGiGUre (cc caccmanssrieacdsigcee se scset dee rade ser i ©
Dera sya Ee VISCUM ES Haars esadeecsdscsereccicasacseesteschbieaeeecseens 15 0
Publications: Quarterly Journal ............... 730) 10 *0
Ba Geological Mapiccsc.cccmss<ccee esis 50 0 O
800 O
Balance in favour of the! Society puis -mascncde-esrisds -eiyseseieseeeme 48 13
£2038 13
0)
==)
1
XXIV -
Income and Expenditure during the
RECEIPTS.
& s. d.\\ Sepssena
Balance at Banker’s January 1, 1870 ....479 15 6
Balance in Clerk’s hands January 1,1870.. 31 0 9
—— 510 16 3
Compositions meceiyed ey ieroct te eee eee 252 0 O
Arrears of Admission-fees ............ .. 566 14 O
Admission-fees, 1870 ........ Walsh gee OL LOO
(0)
Arrears of Annual Contributions .................. 205 11 0O
-Annual Contributions for 1870, viz. :—
Resident Fellows ......... £783 6 0
Non-Resident Fellows ... 45 13 6
ee OO COMES
Annual Contributions in advance.............+-.-e. 17 17 O
Dividends on Consols ........ Sal 6 Aereet enee 160 O10
Journal Subscriptions in advance.................- l* 60
Publications :
Sale of TransactionS......cccccssccccecccs 114 3
Sale of Journal, Vols. 1-25 .............. 107 13 9
i Vol 26") ch Mee es 9913 4
Sale of Geological Map ..-.....-.....-00- 39 2 4
Sale of Library-catalogues ................ 112 6
Sale of Ormerod’s Index..........-.-ceee. 813 0
Sale of Hochstetter’s New Zealand ........ 410 6
262 19 8
We have compared the Books and ve
Accounts presented to us with this VA
statement, and find them agree. Wi
(Signed) Fe Ce Auditors. £2560 16 3
Feb. 6, 1871.
* Due from Messrs. Longman, in addition to the above, on Journal, £8. de
Vol. 26, &C. . ce eee ce ee ee cere n eee cet eee scccces 54 8 1
Due from Messrs. Stanford on Geological IMEIO) ooagobdnbooDoe 13 4 8
Due from Fellows for Journal subscriptions, estimated .... ee: 13 0 0
XXV
Year ending December 31st, 1870.
~
EXPENDITURE.
General Expenditure : £ sda. BEDS Vee eal
HIRAI Seg reraie onckoye i atevavccssecwlete sicvouoveiaialeiareresaletions 41 11 8
HIKESUNSIUANGE! ceicheeucioieretole erelecielaleieraicelevele 6 0 0
INewsBurnifure. cen ocieiaceiseicescieielciereres sis 8 6 0
House-repairs ......ee+e essere cere cee 26.19 9
Hire pees aie soveta: ei ccovsiev cists evovers Se.eeeianeiouel avarehere 27 17 +O
TLRENy SG le I Ue Sareea aa 2513 6
Miscellaneous House-expenses........---- 66 5 1
SHAMOMOA, nooo dcop do ooco 4S bono aoSg0nOS 25 19 10
Miscellaneous Printing, suds Abstracts. 53 17 6
Tea at Meetings bed sade 20 7 O
———. 802 17 4
Salaries and Wages:
Assistant-Secretary ......cc cece cecceens 210 0 O
(yank ae aGaald ach Apacs cas como tonmD oOo 100 0 O
Library and Museum Assistant .......... 59 0 0
POnbeTeretevers i cinie sislsta dis! oiete ee sveie statereiatsvers 100 0 0
PTOUSEMIAIG mre verse tele Soars ack eis laracrerentavelerers 40 0 0
Occasional attendants .........esssseees 8 0 0
WaOWECEOR Wa ek sialon ecvasavole GS alsroteleereteceiets 13) an 3
INC COUNUATI tial ciac erctsisie’s) clalelekarene: shareretelelevare 5. 0 0
— 535 3)
MAT ppecr see cise carta eles! vh fe? sa) cyaseheliore! or age apes S fojehensiee) Sct ois A Lt AG
Miscellaneous Expenses ............ ts 73:16 6
Diagrams at Meetings . En boGe oe Go Us uBloeeosdE 10 6 6
Investment in £211 7s. 3d. Cee ae aa vaaeed sg Wigs ai! 2004 0) 0
Publications :
Geological Map ...... -..0--eeeseceeeee 1617 7
Vournal aVOlseel — 20 lyliaeycreicl) eter selec isye/atter= 915 1
oka MONGTLOO A Rit Ci ayaa AGE ENND 765 14 6
Ormerod’s Index ... Aor 108 5 O
—— 900 12 2
Balance at Banker’s, Dec. 31, 1870 .4388 8 2
Balance in Clerk’s hands, Dec. 31, 1870.. 28 8 10
VOL. XXVII.
——=-— 46617 0
£2560 16 3
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PROCEEDINGS
AT THE
ANNUAL GENERAL MEETING,
170m FEBRUARY, 1871.
AWARD OF THE WoLLAston MEDAL.
Tue Reports of the Council and of the Committees and Auditors
having been read, the President, JosepH Presrwicn, Esq., F.R.S.,
handed the Wollaston Gold Medal to Professor Ramsay, F.R.S.,
F.G.S8., addressing him as follows:—
Prorsssor Ramsay,—I have great pleasure in presenting you with
the Wollaston Medal, which has this year been awarded to you by
the Council of the Society, in recognition of your many researches
in practical and in theoretical geology. Distinguished as your
services have been in connexion with the Geological Survey since
you entered upon it as the Assistant Geologist of Sir Henry De la
Beche in 1841, and more particularly since your appointment as
Local Director in 1845, during which period you have superintended
and carried out the admirably minute style of mapping now general
on the survey, and done so much in training its members in the
field, you have not less distinguished yourself by your investigations
of the higher problems involved in the study of geology. Your first
work was on the Isle of Arran; and although then only a beginner,
you, instead of taking the rocks to be what they looked, worked out
what they were, and gave a new and independent reading of them,
which has since in great part proved to be the right one. In 1846
your well-known memoir “On the Denudation of South Wales and
the adjacent Counties of England” showed the enormous amount of
denudation that the Palwozoic rocks had undergone before the depo-
sition of the New Red Sandstone. At subsequent periods you dwelt
on the power that produced ‘“ Plains of Marine Denudation,” a term
introduced, I believe, by yourself, and showed in all cases, by a
series of true and beautiful sections, how this had operated in
planing across the older strata, and how valleys had been scooped
out by subsequent aqueous causes in the great plains so formed.
¢2
XXVIII PROCEKDINGS OF THE GEOLOGICAL SOCIETY.
Whilst unravelling the complicated interior phenomena of fhe
Welsh rocks, you were not unmindful of the very different order of
phenomena exhibited on their exterior surfaces. Here you showed
the vast extent and power of ice-action, and what a glacier-land
Wales once was. Reasoning from the present to the past, you also
boldly pushed your ice-batteries far back into geological time, and
were the first to bring them to bear on rocks of Permian age. That
advanced post you long had to hold alone ; but other geologists have
since followed your lead, and we have even lately had evidence in
the same direction from Southern Africa, where it is asserted that
boulders and glaciated surfaces have been found at the base of the
Karoo formation of supposed Triassic age. ;
You have also held a prominent place among those who, by their
public teaching, have done so much during the last twenty years to
advance the cause of our science. To myself personally, whose
geological career has run nearly parallel in time with your own, it
is a source of much pleasure that it has fallen to my lot to hand you
this the highest testimonial the Society has to bestow.
Prof. Ramsay made the following reply :—
Mr. Prestpent,—I cannot say whether I am more pleased or
surprised by the unexpected award to me of the Wollaston Medal
by the Council of this Society. Pleased I well may be, not because
I ever worked for this or any other honour, but because I feel a
sense of satisfaction that the work on which I have been engaged
for the last thirty years has been esteemed by my friends and fel-
lows of the Council of the Society so highly that they have deemed
me a fit recipient of this honour. It is also a special satisfaction to
me that this award has been bestowed by the hand of one of my
oldest geological friends, who is so universally esteemed and beloved,
and is himself so distinguished a contributor to physical and other
branches of our science.
My first endeavour in geology (the construction of a geological
map and model of Arran) necessarily drew my attention to the
physical part of our science ; and when, consequent upon that work,
I was, through the intervention of my old and constant friend Sir
Roderick Murchison, appointed by Sir Henry De la Beche to the
Geological Survey of Great Britain, my whole subsequent life was
thereafter necessarily involved in questions of physical geology ; for
no man can work on or conduct the field-work of such a survey who
does not, aided by paleontology, necessarily make that his first aim.
4 .
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXIX
If some of my theories, induced by that work, were long in being
recognized, the recognition has been all the more welcome when it
came. Probably I never should have been able to do what I have
done but for the wise example of my old master Sir Henry himself,
in his time the best thinker in England on the physical branch of
our science, and to whose remarkable work, ‘ Researches in Theo-
retical Geology,’ all geologists are to this day indebted.
The papers which I have written are mere offshoots from my
heavier work on the Geological Survey. Perhaps they are enough
for the readers; but I wish they had been more numerous, for I
certainly have had many more in my mind. ‘Two of these, on old
physical geographies, I have lately given to the Society ; and if they
should be printed, I shall be well pleased should they soon or late be
found worthy. The present physical geography of the world is but
the sequel of older physical geographies ; and to make out the history
of these is one of the ultimate aims of geology. These are the sub-
jects I have striven to master in part. I consider your award a
sign that I have had some success; and if, before I cease to work,
I have a little more, I may well be content.
AWARD OF THE WoLLASTON DonATION-FUND.
The President then presented the Balance of the Proceeds of the
Wollaston Donation-fund to Rosrrr Eraeriner, Esq., F.G.S., in
aid of the publication of his great stratigraphical Catalogue of
British Fossils, and addressed him as follows :—
Mr. Erxeriper,—The Council of the Society has awarded to you
the Proceeds of the Wollaston Fund, to aid in prosecuting your
valuable work on the fossils of the British Islands, stratigraphically
arranged. In this work, on which you have been engaged during
the last nine years, and which occupies nine volumes of MS., repre-
senting as many geological groups, you give the natural-history lists
of each group, and trace the history of each species both in time and
space. Of the magnitude of the work few can have any idea; nor
would many have an idea of the marvellous extent of past life in
our small portion of the globe without a comparison of our recent
fauna with those (necessarily incomplete because only partly acces-
sible) which you have enumerated in your most useful lists. This
comparison shows :—
xxx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
a
oa Bg * Ss
S Bee ag § S rc -
SEeee! pa: ae
Spaad Sly ing ae 5 & Total.
AOR OO & & & a a &
——
Number of Species in
the existing fauna and + 616 278 567 263 15 354 76 1820 3989
flora of Great Britain
Number of Species
found fossil in Great $ 2574 746 7091 815 224.12 172 819 12453
Britain! tosnwe west enecne
I trust that this work will not be allowed to remain in MS., and
that, presuming you will begin with the oldest, we may soon look
for an instalment in the fauna of the Paleozoic rocks. I have
much pleasure in presenting you with this token of the importance
which the Geological Society attaches to your labours,
Mr. Ernrriner made the following reply :—
I have great satisfaction in receiving from you, Sir, and the
Council of the Geological Society, the award of the Wollaston-fund.
It is given for work known to be nearly done, and faith in its com-
pletion. The time and labour devoted to my book upon the ‘ Stra-
tigraphical Arrangement of the British Fossils’ has extended over
nearly nine years of incessant work, and has been an arduous yet
pleasant undertaking, now made lighter by the recognition of those
who know and value the researches made for so extensive a
catalogue of the British organic remains, now numbering nearly
13,000 species. It is this estimation of my labour by the Council
and Society that tends to increase the desire to make my work as
perfect as possible, well knowing how difficult, if not impossible, it
is to doso. This acknowledgment, Sir, from your hands will stimu-
late me to complete my researches into the literature of the British
species, and trace their history through space and time throughout
HKurope.
THE ANNIVERSARY ADDRESS OF THE PRESIDENT,
Josppa Prestwicn, Ksq., F.R.S.
GrntLEmMEN,—I have to congratulate you on the Report of the
Council, which announces the flourishing state of your finances, the
addition to your number of Members, the extension of your library,
and the increasing importance of your Journal.
* Testaccous species only.
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXX]
It is my duty first to mention those of our fellow-workers whose
loss during the past year we have to deplore. Although the number
of deceased Members amounts to 23, there are but few whose active
cooperation in the special work of the Society has to be recorded.
The name of Rozert Huron is associated with the earliest days
of this Society, of which he was elected a Fellow in 1813. He spent
the early years of his life in Dublin, which city he represented in
Parliament from 1837 to 1841. He was the friend and associate of
Greenough, Buckland, and other founders of this Society, in the
proceedings of which he ever took the warmest interest. During
various excursions through Ireland, he made a considerable collec-
tion of minerals and fossils, which, on his leaving Dublin in 1836,
he presented to the Geological Society of Dublin, of which he had
been a member since its commencement in 1832. In 1836 he was
placed on the Council of our Society, in 1837 served as Secretary,
and was one of the Vice-Presidents in 1845 and 1846. He took
for many years an active part in the Society, but did not contribute
any thing from his pen, although always ready to assist others by
his advice and countenance. He was also one of the original pro-
moters of the London University (now University College), and was
on its Council for 30 years. He was born in 1784, and died in
August 1870.
Coronet Sir Prosy T. Caurtzey, K.C.B. In 1831 four young
men, all of whom subsequently became eminent and distinguished,
met, at the commencement of their professional and scientific career,
at a remote up-station in India. Sir Proby Cautley, General Sir
Henry Durand (whose untimely death the nation has had so recently
to deplore), General Sir William Baker, Member of Council of India,
then lieutenants in the army, and the lamented Hugh Falconer, had
their attention drawn by the first-named and by an Indian Prince
to the rich stores of mammalian remains in the Tertiary deposits of
the Sewalik Hills. They all entered zealously upon the investiga-
tion of this new and unexplored ground; and, as Dr. Murchison
observes, “by the joint labours of Cautley, Falconer, Baker, and
Durand, a subtropical mammalian fossil fauna was brought to light,
unexampled in richness and extent in any other region then known.
It included :—the earliest discovered fossil QuapRUMANA; an ex-
traordinary number of Proposcrpra belonging to Mastodon, Stego-
don, Loxodon, and Huelephas ; several extinct species of Rhinoceros,
Chalicotherium ; two new subgenera of Hippopotamus, viz. Heaa-
XXXil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
protodon and Merycopotamus ; several species of Sus and Hippohyus,
and of Equus and Hippotherium ; the colossal ruminant Sivatherium,
together with fossil species of Camel, Giraffe, Cervus, Antilope,
Capra, and new types of Bovide ; Carnwora belonging to the new
genera Hycnarctos and Enhydriodon, and also to Drepanodon, Felis,
Hyena, Canis, Gulo, Lutra, &c. ; among the Aves, species of Ostrich
Cranes, &c.; among the Reptilia, Monitors and Crocodiles of living
and extinct species, the enormous Tortoise, Colossochelys Atlas, with
numerous species of Hmys and Trionyx; and among fossil fish,
Cyprinde and Siluride. The general facies of the extinct fauna
exhibited a congregation of forms participating in European, African,
and Asiatic types. Of the mammalian remains all belonged to ex-
tinct species; but of the Reptilia and freshwater Shells some of the
fossil species were identical with species now in existence on the
continent of India: and from this fact, more than thirty years ago,
Dr. Falconer was led to draw important inferences as to the antiquity
of the human race” *.
Joint notices of these remarkable discoveries were sent in from
time to time and published in your ‘ Transactions.’ Independently
of these, Sir Proby Cautley communicated to the Society separate
papers “On the Structure of the Sewalik Hills, and the Organic
Remains found in them,” and “ On the Finding of the Remains of a
Quadrumanous Animal in the Sewalik Hills,” whilst several others
bearing on the same subject were published in the Journal of the
Asiatic Society of Bengal, and elsewhere. These researches were
continued by Sir Proby and Dr. Falconer during eight years with
indefatigable perseverance and at great expense; in 1840 Sir Proby
sent this unrivalled collection, which filled 214 cases, each weighing
about 4 cwt., to England. This collection was offered to our Society ;
but for want of room it had to be declined, and it was placed in
the British Museum. It was the intention of Messrs. Falconer and
Cautley to describe and illustrate the whole of their large collec-
tions in a magnificent work entitled ‘Fauna Antiqua Sivalensis,’ of
which 9 parts were published, but which, to the regret of the
scientific world, yet remains to be completed.
In 1837 the Wollaston Medal was awarded in duplicate to Sir
Proby (then Captain) Cautley and Dr. Falconer “ for their geolo-
gical researches and their discoveries in fossil geology in the sub-
Himalayan Mountains.” Although an artillery and not an engineer
officer, Sir Proby’s abilities were so highly valued that he was ap-
* «Paleontological Memoirs’ of Hugh Falconer, vol. i. p. 28.
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXili
pointed in 1841 to construct that important work the Ganges Canal.
This difficult and great public work, probably the greatest then exe-
cuted under British rule in India, its main channels being 820 miles
in length, was equally to the honour of those who promoted and of
him who projected and successfully carried it out. It was completed
in 1854. Soon after this, Col. Cautley returned to England, where
he was made a K.C.B., and in 1858 he was selected to fill one of the
new seats in the Indian Council, which he held till 1868, when he
retired into private life after a service of 50 years. Sir Proby
Cautley was born in 1802, elected a Fellow of this Society in 1836,
and died last month at his residence in Sydenham.
In Lorp Carer Baron Srr Freperick Pottock, Bart., we have
lost another early and distinguished Fellow. He was elected in
1818. I cannot ascertain that he ever wrote on any geological
questions ; but the Transactions of the Royal Society are enriched
with several memoirs by him on the curious peels connected
with mathematical theories of numbers.
Dr. Cottier joined the Society in 1838. In early life he saw
much of the world as a staff-surgeon in the army, and paid particular
attention to the conchology of Ceylon when stationed there. He
was also eminent as a Greek scholar. He died last May at the
advanced age of 86.
In Mr. Braprorp the Society has lost a promising young Member,
who took first-class honours in Natural Science at Cambridge, and
afterwards during five years taught English Literature and Science
at Hooghly College in India. He died at the early age of 32.
The Rev. C. Erte was elected a Fellow of the Society in 1837.
For many years he was a very constant attendant at the evening
meetings, and he will be remembered by many for the pleasant part he
took in some of our discussions. He travelled much in France and
Italy, and paid great attention to the volcanic phenomena of those
countries. In 1833 he was appointed to the living of Hardwich, near
Aylesbury, where he resided till his death last year. Of the Saurian
remains of that district he made a large collection. Mr. Erle was also
a distinguished classical scholar. He was born in 1790.
Amongst our foreign Members, science has sustained a great loss
in Professor Gustav Biscnorr, of Bonn, who died last year at, the
age of 78. At an early period of his life, he devoted himself to
Chemistry and Physics; and his attention becoming afterwards di-
XXXIV PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
rected to Geology, a science then in its infancy, he brought his
knowledge of chemistry to bear upon the many difficult and inter-
esting problems of Chemical Geology. In 1826 he published a
paper “Sur Vorigine des sources Minérales.” In 1827 a paper
“Sur les efflorescences des Roches Volcaniques.” These were followed
by various papers on Fossil bones, the inflammable gases of Coal-
mines, Volcanic rocks, Glacier action, and others in the « Neues Jahr-
buch.’ Many of his papers appeared in the ‘ Edinburgh New Philo-
sophical Journal ;’ amongst them are to be found “ On the Natural
History of Volcanoes and Earthquakes,” “On the Terrestrial ar-
rangements connected with the appearance of Man on the Earth,”
‘On the cause of the Temperature of Hot and Thermal Springs, and
on the bearings of this subject as connected with the general ques-
tion regarding the internal temperature of the Karth.” He also
treated of ‘“ The Glaciers in their relation to the elevation of the
Alps,” and of “The Formation of Quartz and Metallic Veins.”
Most of his early papers were afterwards embodied in his great
work the ‘Lehrbuch der chemischen und physikalischen Geologie,’
which appeared between 1847 and 1854. In the latter year a trans-
lation of this work by Dr. Paul and Dr. Drummond, made under the
supervision of the author, was published by the Cavendish Society.
This important work, more condensed than the German edition, is
in some respects an independent work. In the first volume, the
laws of combination of the mineral kingdom, pseudomorphic minerals,
the action of water as a chemical and a transporting agent, the
origin of springs, the action of rivers and of the sea, the mechanical
and chemical deposits from water, and the character and origin of
carbonaceous substances, of various gases, and of the simple salts
occurring in the mineral kingdom, are treated of; while in the
second the chemical reactions relating to the alteration of minerals, and
the characters of and changes in Felspathic andvarious other minerals,
especially those of volcanic and igneous origin, are considered. No
geological studies can be complete without a knowledge, at all events,
of the elements of Chemical Geology. In 1861, Professor Bischoff
was elected a foreign Fellow of this Society ; and in 1863 the Wollas-
ton Medal was awarded to him by the Council, in recognition of the
eminent services rendered by him to Geological science by his long-
continued and laborious chemical investigations on the origin and
changes of minerals and rock-substances, and especially by the pro-
duction of his great work on Physical and Chemical Geology.
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV
Many of the papers read during the past year have been of much
interest and well serve to maintain the character of our discus-
sions and publications. Those connected with glacial and drift-
action continue to occupy an important place.
Glacial and Tertiary Geology.
The Rev. W. Bleasdell shows how a small island in the St. Law-
rence has been removed piecemeal by river-ice floating off detached
portions during floods ; and Dr. Brown applies the result of his ex-
_ perience in the arctic regions of America to the explanation of the
glacial phenomena of Scotland, the sub-azoic Boulder-clay of which
country he considers analogous to the deposit under the ice-cap of
Greenland, while the associated fossiliferous laminated clays were
formed in the fiords and bays skirting the ice-covered land.
Professor Harkness objects to former hypotheses respecting the
distribution of the Shapfell Granite boulders over the high hills of
Yorkshire, and suggests that their transport could only have been
effected by the agency of coast-ice during a depression of the land of
1500 feet.
The superficial drift-deposits of South Hampshire and the Isle of
Wight have been carefully investigated by Mr. Codrington, who
shows that the unfossiliferous gravels of the higher plains were
probably not of river-origin, but were spread out in an inlet of
the sea, when the land stood 400 feet lower, whilst the gravels on
the lower levels, with mammalian remains and flint implements,
were afterwards deposited by river-action.
Mr. De Rance has described the Preglacial and Glacial deposits
of Western Lancashire and Cheshire. He considers that at the
commencement of the Glacial period the land stood higher than it
now does, and that the higher ground was covered with an ice-
cap and great glaciers, that the higher Boulder-clay is referable to
this land-ice, and that the lower Boulder-clay spread over the lower
ground was formed during a period of subsidence when the land-
ice was floated off. He infers also that, when the land stood higher,
‘Treland would haye been connected with Wales, so as to render
possible the migration of mammals and plants.
Mr. Searles Wood, jun., has reviewed the vexed question of the
origin of the Weald Valley, and doubts the sufficiency of the various
hypotheses that have been proposed to explain the denudation of
that district. From the comparative absence of Lower Cretaceous or
Wealden débris in the Thames valley, and the presence of Tertiary
XXXV1 PROCEEDINGS OF THE GECLOGICAL SOCIETY.
pebbles in gravels within the Wealden area, and the manner in which
the transverse valleys open out, estuary-shaped, into the Weald,
he infers that that was occupied in Postglacial times by an inlet
of the sea, into which rivers flowed from the Thames-valley area,
and that the denudation was chiefly effected by tidal erosion during
a gradual upheaval of the land.
The Rev. John Gunn is now of opinion that the ‘* Forest-bed
series,” which he has so long and carefully studied, is older than the
Norwich Crag and the Chillesford Clays, and that the latter covers
both the other deposits transgressively in proceeding from the coast
toward the interior of the country.
Mr. Ray Lankester has made further contributions to our know-
ledge of the Crag-beds of Norfolk and Suffolk. He considers that
the Stone-bed at the base of the Norwich Crag is not identical with
the Bone-bed at the base of the Suffolk Crag, and shows the marked
difference in their mammalian fauna. The Rhinoceros, Tapir, Hip-
parion, and Hyzna of the Bone-bed are introduced Miocene
species ; while the Elephants and Deer of the Stone-bed and Forest-
bed are of Pliocene species not found in the Bone-bed. He de-
scribes from this latter bed a new ziphioid cetacean, and has deter-
mined the presence of Mastodon arvernensis in a sandstone nodule
found in it. Of these nodules Mr. Lankester gave additional par-
ticulars, showing, by their organic remains, their derivation from
beds of ‘‘ Diestien”’ age.
In making excavations for the extension of the dockyard in
Portsmouth Harbour, a fine section of the Lower part of the London
Clay, with overlying gravel and alluvial beds, has been exposed ;
and a good account has been given of them by Mr. C. J. A. Meyer.
Some of the beds are very fossiliferous, and contain an assem-
blage of species which have not been found elsewhere in the London
Clay: one of the species is a Thanet-sand form, while another is the
well-known Cardita planicosta of the Bracklesham beds and of the
Calcaire grossier.
Secondary Formations.
The only communications we have had on the Cretaceous series
are as follows. Mr. Whitaker describes the divisions of the Chalk of
the south coast. He shows that the Chalk Marl and Lower Chalk
thin westwards, while the Upper Chalk with flints passes trans-
gressively over and beyond it, and thus are flints found so far west.
Mr. Judd gives the result of his further examination of the Neoco-
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXVI1
mian beds of Yorkshire and Lincolnshire, and shows their relation
to those of Hanover, Westphalia, and Brunswick. The Speeton-
clay series he considers to be the keystone in the correlation of the
beds over the whole area.
In a subsequent paper Mr. Judd gave an interesting account of a
series of beds between the Neocomian and Wealden strata of the
south coast. The section where they were first noticed some years
since by Mr. Godwin-Austen and Prof. E. Forbes is at Punfield, in
the Isle of Purbeck, whence Mr. Judd suggests the name of ‘ Punfield
Formation” for these beds, which he shows to be of considerable im-
portance, having a wide range through France, and being closely
related to the coal-bearing strata of the north of Spain described
by M. de Verneuil. The fossils are mixed and of a peculiar type;
and there are many species common to the English and Spanish
series.
Mr. 8. Sharp subdivides the Oolites of the Northampton district,
and shows that the line of division between the Great and the In-
ferior Oolites in the neighbourhood of Northampton is marked by
unconformity as wellas by organic remains. He states that there are
four areas, within a comparatively small space, in which the whole
of the beds occurring in each, from the Great Oolite down to the
Upper Lias inclusive, are accessible. The Northampton Sands he
proposes to class in three divisions—the Upper, Middle, and Lower.
Though the beds vary considerably in thickness, according to the
different localities, the total thickness of the Northampton Sands
may be taken on an average as about 80 feet.
Mr. Mitchell suggests that the valleys of the Oolitic district round
Bath are due not so much to denudation as to the circumstance that
many of the beds of Great Oolite are old coral-reefs of limited ex-
tent, while the argillaceous strata are true sedimentary deposits
overlying and wrapping round them, so that the Oolitic beds never
in fact extended across the present valleys, though the clay beds did.
Mr. R. Tate continues his researches on the fossils of the different
divisions of the Lias in Gloucestershire, and shows the value of the
Ammonite-zones over certain areas—also that although the condi-
tions of depth and deposit of the upper part of the Lower Lias are
repeated in the lower part of the Middle Lias, there is a total change
in the fauna, whence he infers a break in the stratigraphical suc-
cession.
Prof. Ramsay states, in an interesting paper “‘On the physical
Relations of the New Red Marl, Rhetic Beds, and Lower Lias,” that
XXXVIll1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
there is a perfect physical gradation between the first two. He
considers that the New Red Sandstone and New Red Marl were
formed in inland waters—the latter in a salt lake of great extent.
These conditions, and the abundance and peculiar condition of the ~
oxide of iron, would, Prof. Ramsay thinks, be in accordance with those
chemical characters of the waters, while he considers that the fossil
footprints occurring in these beds are evidences of the absence of
tides in the waters. He gives stratigraphical and paleontological
reasons in proof of the New Red Marl being more closely related
to the Rhetic beds, and even to the Lias than to the Bunter, and
traces the sequence of events during the accumulation of these
several formations.
Paleozore and Metamorphic Rocks.
From Dr. Nicholson we have a paper on a part of the “ Lower
Green-slates and Porphyries” of the Lake district. They were so
named by Prof. Sedgwick, and underlie his Skiddaw Slates. Over
these are felspathic rocks, succeeded by a series of ash-beds, brec-
cias, and amygdaloids, which are often worked as slates.
Mr. Jamieson divides the older rocks of Banffshire into three
groups :—first, a lower arenaceous series more or less altered by
metamorphic action into quartz-rock, gneiss, and mica-schist ; next,
a series of clay slates, with a subordinate bed of limestone ; thirdly,
an upper group of areraceous strata. A main object of his commu-
nication is to give his reasons for considering that the granites of
Banffshire are due to the fusion and recrystallization of the arena-
ceous beds.
Paleontology.
In the paleontological papers,—
Mr. Busk has pointed out that the Oreston fissure-cavern Rhino-
ceros is not the &. tichorhinus, but R. leptorhinus.
Three species cf Elephant are now ascertained to have lived in
Malta during the Cave-period. Dr. Caruana draws attention to the
abundance of their remains in a particular part of the island, in-
cluding one new locality.
Mr. Hulke has described an Ichthyosawrus supposed to have been
found in the Isle of Gozo; and if so, it is the first one discovered in
beds of Tertiary (Hocene?) age. He has also described two species
of Plesiosaurus from the Kimmeridge Clay of Dorsetshire; one of
these is a slender-necked species 16 feet in length, and with Plio-
saurian-like limbs, which are much larger, compared with the whole
length, than those of the typical Liassic forms of this genus.
ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXIX
Professor Huxley communicates a letter from Dr. Bunzel, of
Vienna, giving an account of a skull of Cretaceous age, belonging to
a new order of reptiles with bird-like heads, for which the author
proposed the name of Ornithocephala.
Messrs. Hancock and Howse describe a new Labyrinthodont am-
phibian from the Magnesian Limestone of Durham, and a new
Proterosaurus (P. Hualeyi) from the marl-slate of the same district,
associated with the P. Speneri. They also announce the discovery
in the same rock of specimens of that peculiar fish the Dorypterus
Hofmanni, showing the ventral fins and heterocercal tail.
A very interesting paleontological discovery has also been made
by Mr. Maw of a fine skull of a Labyrinthodont in the middle of the
Coalbrook-Dale Coal-measures.
Mr. H. Woodward has drawn attention to some new Crustaceans,
including a species of the curious Secondary genus Palwocorystes, and
also to two new forms referable to the family of Portunide, in the
lower beds of the London Clay of Portsmouth, of which the sec-~
tion has been described by Mr. Meyer. Mr. Carruthers has de-
scribed a silicified fern-stem, probably from the sands under the
London Clay at Herne Bay. In structure this specimen agrees most
closely with the living Osmunda vegalis. The minutest structure of
the original specimen is preserved in a remarkable manner, even
showing the starch-grains and the delicate mycelium of a fungus
contained in its cells.
Colomal and Foreign Geology.
We have had some excellent papers on Colonial Geology ; and we
are especially indebted to our correspondents in South Africa.
Dr. Sutherland describes an ancient Boulder-clay in Natal. It is
an argillaceous deposit with boulders, reposing upon old sandstones,
the surface of which is often deeply grooved and striated. He con-
siders that this deposit may possibly be of Permian age.
Mr. G. W. Stow describes the Jurassic beds (with their Trigonia-
limestones) and the Saliferous beds of Uitenhage, between the Cape
and Natal. These are succeeded by Tertiary deposits, the newer
of which follow the coast-line, and run in raised terraces up the
river-valleys—the one being characterized by a large Panopea,
and the other by a species of Akera. The Karoo formation of the
Stormberg, which is of Triassic age, with its plant-beds and Dicyno-
dont fossils, are described in another memoir. The present sur-
face-conditions of this part of the interior Mr. Stow considers espe-
x PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
cially due to ice-action; and he points also to the existence of
Roches moutonnées and moraines in British Kaffraria and adjacent
districts.
Mr. C. L. Griesbach has given an excellent account of Natal,
and describes the succession of beds, commencing with the granitic
and gneissic rocks and mica-schists, overlain by great plateaux of un-
disturbed sandstone, often capped by basalt. The sandstone is suc-
ceeded by the Karoo formation, containing occasionally subordinate
beds of coal, and then near the coast by beds of Cretaceous age.
Reference is made to various interesting theoretical questions con-
nected with the former distribution of land and water between
Africa and India, and to the economical mineral products (graphite,
coal, gold, and copper) of Natal.
Some notes on the Diamond districts of the Cape of Geral Hebe
have been given us by Mr. Gilfillan.
We have had only one communication from Australia, by Dr.
Krefft, on certain of the later fossil Mammalia, including several
species of Wombats and Wombat-Kangaroos of that remarkable
continent.
The relations of the two gneissoid series of rocks of Nova Scotia
have been discussed by Mr. H. Youle Hind, who believes them to
be of Laurentian age, and covered in patches only by the Huronian
or Cambrian rocks. The gold is found in Lower Silurian rocks,
which formation is there 1200 feet thick, and is destitute of any
great beds of limestone.
The Rey. T. G. Bonney describes the general appearance of the
Lofoten Islands. Instead of being composed of granite, he thinks
that, with few exceptions, the strata consist of highly metamorphosed
rocks—quartzites and gneiss.
Foreign Paleontology.
Professor Owen has described some fossil mammals of late Ter-
tiary or Quaternary age found in China. Among them are new
species of Stegodon, Hyena, Tapir, Rhinoceros, and Chalicotherrum.
Principal Dawson has sent us the result of his further examina-
tion of the structure of the Sigillaria, Calamites, and Calamoden-
dron of the Nova-Scotia Coal-field. A specimen of Sigillaria was
described having a transversely laminated pith of the Sternbergia-
type, the immediately surrounding tissues much resembling those
of Cycads. He agrees with the opinion generally held with re-
gard to Calamites, that their affinities were with Hquwisetacee, as
ANNIVERSARY ADDRESS OF THE PRESIDENT. ‘xii
pointed out by Mr. Carruthers, but more advanced than the modern
Liquseta, while the Calamodendra were similar in general structure,
but much more woody plants.
Professor Heer has described the flora of Bear Island, in latitude
74° 30'N. He considers it to belong to the lower part of the Car-
boniferous series. There are eighteen species of plants, having a
close relation with those of the Yellow Sandstones of county Cork and
of the Greywacke of the Black Forest. Taking also the fossil flora
of Parry Island and Melville Island, which he considers the equiva-
lent of that of the Bear-Island beds, we have a total of 77 species
of plants. Not less remarkable than the occurrence of this rich and
luxuriant vegetation in those arctic regions during this Carboni-
ferous period, is the appearance of a flora equally rich and varied, in
the same regions, in the comparatively recent Miocene times.
Mr. Billings has made in the Lower Silurian rocks of Canada the
interesting discovery of a Trilobite (Asaphus platycephalus) with its
appendages preserved and the hypostome in position. It shows
that the creature had eight pairs of legs; so that probably these
Crustacea were walking rather than swimming animals. Mr.
Woodward has found in a specimen presented some years since to
the British Museum by Dr. Bigsby traces of similar appendages.
He considers that the Trilobita should now be placed newt to, if
not actually with, the modern Isopoda.
Dr. Grey has sent us some interesting specimens of Dicynodont
fossils, jaws of reptiles, and coal-plants, from the Karoo beds of
South Africa.
Mr. Guppy is of opinion that he has detected an Hozoon, with a
coral and echinoderms, in some Trinidad rocks, the age of which is
uncertain, but considered by the author to be pre-Silurian.
The PatzontrocrapuicaL Society continues its valuable publica-
tions. The vclume for 1870 contains the concluding part of Mr.
Davidson’s great work on the Brachiopods. It completes the Silu-
rian Brachiopoda, consisting of 28 genera and 210 species, while the
whole work, by that author, forms three volumes, with 150 plates,
all of which have been drawn and contributed by Mr. Davidson
himself. Another paper of importance is the complete monograph
of British Mesozoic Mammals by Prof. Owen, containing descriptions
and illustrations of 15 genera and 27 species.
Independently of your own Society, the progress of geology is
being actively advanced by local societies, the number of which is
VOL, XXVII. d
xii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
annually increasing. Many of them publish Proceedings of consider-
able merit; and others tend, by field-work, to spread a taste for
your science.
Deep-sea Life and its Relations to Geology.
Among the collateral subjects which have engaged much at-
tention during the past year, and which must exercise a consider-
able influence on future geological speculation, is that relating to
the nature of the sea-bed, the temperature of the sea at great
depths, and the range and distribution of animal life in those depths—
investigations which have been so greatly promoted by the recent ex-
peditions of H. M. surveying-steamers ‘ Lightning’ and ‘ Porcupine.’
Subjects of this nature have always been of much importance to
the geologist, who has therefore ever followed with the keenest in-
terest the researches of the naturalist and physicist. In studying
the marine Invertebrata the early naturalists were long limited in
their observations to the shore-line, and to such moderate depths as
were within reach of the ordinary fishermen or their own small ap-
pliances. Now and then a deep-sea sounding would give a frag-
mentary insight into other zones of depth; but from their excep-
tional character they did not attract much notice. Lamarck, O. F.
Miller, Montagu, Poli, and Risso furnished some facts relating to
depth as well as to geographical distribution ; but still, when we
look to the short table by Mr. Broderip of the “ Situations and Depths
at which recent Genera of Marine and Estuary Shells have been
observed,” appended to Sir Henry de la Beche’s ‘ Theoretical Geo-
logy,’ it shows how scanty our information was so late as the year
1834. No Mollusca are there given from a depth greater than
420 feet, and no Brachiopcda from one greater than 540 feet.
In the various inquiries which engaged the attention of the emi-
nent men who formed part of the many Arctic expeditions, that
of the distribution of life in the sea was not lost sight of, although,
from the imperfection of the means, the results were very scanty.
The small quantity of mud or stones attached to the sounding-
apparatus, or brought up by the deep-sea clam, furnished, in fact,
all the glimpses they were able to obtain of the ocean-bottom.
Although the specimens were often crushed and broken, still the
evidence, so far as 1t went, was in many cases clear and definite.
Sir John Ross records, in his voyage to Baffin’s Bay in 1817—
18, three deep-sea soundings. In the first, at a depth of 2700 ft. *,
* I have in all cases expressed the sea-depth in feet instead of in fathoms,
in order to conform with the terms applied to elevations on the surface and
dimensions of strata.
ANNIVERSARY ADDRESS OF THE PRESIDENT. xiii
and two miles off shore, they brought up gravel and two small live
crustaceans (Gammarus); in the second, in 3900 ft. and eighteen
miles off shore, pebbles and brown clay, with Serpule, corallines,
crustaceans, and fragments of shells ; in the third, in 6000 ft. and six
miles off shore, soft mud, with some worms in it. Again, in a sound-
ing where the depth was 6300 ft., a small starfish was found at-
tached to the line below the point marking 2400 ft.
Mr. Alex. Fisher, in his account of the voyage of the ‘ Hecla’
and ‘Griper’ in 1819-20, states that, in a sounding taken on ap-
proaching Lancaster Sound, they brought up from a depth of
5100 ft. mud, with small stones and pieces of prepen shells of very
delicate texture.
A curious case is recorded in the voyage of the French frigate
‘Venus,’ in the Pacific, by M. de Tessan in 1838. When near
the Equator, a bottle full of fresh water and well corked was at-
tached to the sounding-line near the lead, and let down to the depth
of 7500 feet. The bottle came up with the cork forced in, and
containing a small living shell of the genus Venus.
Sir James Ross, in his voyage to the Southern and Antarctic ‘Seas,
in 1839-43, obtained more definite results. At a depth of 1800 ft.
he found “ corallines and many animals ;” at 1920 ft. “ green mud,
with a fragment of starfish and coral;” while the result of a haul
2400 ft. deep, subsequently examined by Mr. Charles Stokes and
Edward Forbes, showed the presence of small corals, pieces of
shells, and two joints of a small fossil (?) Pentacrinite, a spine of C1-
daris, portions of Echinus, a small broken Cerithium, a fragment of
Cleodora, and specimens of Spirorbis on some stones. With these
there were Foraminifera of the genera Zextularia, Nodosaria, and
some others, in abundance.
That the specimens brought up on these occasions were generally
fragmentary was almost to be expected.
With the application of the dredge to the purposes of deep-sea
exploration, materials. for a more exact classification of species ac-
cording to their bathymetrical range rapidly accumulated ; and in
the year 1839 a Committee of the British Association was appointed
to carry out a systematic investigation of the seas of the British
coasts. In 1840, Prof. E. Forbes, then about to join the surveying-
ship ‘ Beacon’ as naturalist, was requested by the Association to
furnish them with a report on the Mollusca and Radiata inhabiting
the Aigean Sea. ‘This report * marks an epoch in Natural History
and Geology.
: * Brit. Assoc. Reports for 18438, p. 173.
d 2
xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Besides giving the lists and range in depth of the Mollusca and
Radiata, the Report entered into the question of their distribution
considered in its bearing on geology. The observations of Prof.
Forbes ranged over a period of eighteen months; and his lists are
based on more than 100 fully recorded dredging-operations in va-
rious depths from 600 to 780 ft., besides numerous coast-observa-
tions. The result of this valuable and special inquiry was to de-
termine more clearly than had hitherto been done the range of species
in depth, and the division into zones first proposed by Risso. With
regard to much that Prof. Forbes accomplished no question has
arisen. Of the eight zones into which he divides the bathymetrical
distribution of the Mollusca, the first seven, ranging trom the surface
to the depth of 630 ft., although possibly too much subdivided, may be
applicable to other seas where the conditions are similar ; but with
respect to his eighth region, which extends from 630 to 1380 ft.,
Prof. Forbes’s generalizations, although correct within certain areas,
have been found inapplicable to the two great oceans and applicable
only to parts of the Mediterranean. He observes, speaking of this
eighth zone, “throughout this great and, I may say, hitherto unknown
province, we find an uniform and well-characterized fauna;”’ but
then he goes on to say, “‘ within itself the number of species and of
individuals diminishes as we descend, pointing to a zero in the
distribution of animal life as yet unvisited.” He placed this zero at
about 1800 ft.
- In a subsequent work *, however, in speaking of the eighth re-
gion of depth, E. Forbes remarks, ‘its confines are yet unde-
termined, and it is in the exploration of this vast deep-sea region
that the finest field for submarine discovery yet remains.” “In
the Mediterranean, as might be expected, when we consider the pe-
culiar condition under which that great land-locked basin is placed,
there are peculiarities in the distribution of both animal and vege-
table life which require special consideration ;” and in speaking of
animal life in the “Arctic province” of the Atlantic, he notices
that the Mollusca appear to range much deeper in high latitudes
than they do in more favourable climates, and mentions the ca-
pital haul made by Mr. Harry Goodsir in Davis’s Straits, when
a variety of shells, Crustacea, Echinoderms, and Corallines were
brought up from a depth of 1800 ft.
In another Report}, on British Marine Zoology, E. Forbes di-
vided the range of the Mollusca into only four zones of depth ; and
* Natural History of European Seas, p. 27. Tt Brit. Assoc. Rep. 1850.
ANNIVERSARY ADDRESS OF THE PRESIDENT. xlv
speaking of the fourth or lowest, he observes, “ A more difficult
task, and which can be hardly hoped for fulfilment without the
aid of a steam-vyessel and continued calm weather, is the dredging
of the deeps off the Hebrides in the open ocean. Much of the deep
sea round the Zetlands is sure to reward the explorer.... And lastly,
though I fear the consummation, however devoutly to be wished
for, is not likely soon to be effected, a series of dredgings between
the Zetland and the Faroe Islands, where the greatest depth is under
700 fathoms, would throw more light on the natural history of the
North Atlantic and on marine zoology generally, than any investi-
gation that has yet been undertaken.”
All who knew Edward Forbes must feel satisfied that, had his
valuable life been spared, he would have been in the foremost rank
of the investigators‘of those new fields to which he pointed, and the
exploration of which has now been so successfully commenced. His
untimely death unfortunately left his investigations with all the
weight of his authority, at a point that he doubtless would have
considered the first stage in the inquiry, instead of being accepted,
as it has occasionally been, as an approximate conclusion.
In 1846, Capt. Spratt, R.N., the friend and companion of Forbes,
dredged at a depth of 1860 ft., forty miles east of Malta, eight
distinct species of Mollusca, among which was the Pleurotoma
carinata *, a supposed extinct species of the Coralline Crag; and
he observes + that he believed animal life to “ exist much lower,
although the general character of the A.gean is to limit it to 300
fathoms.” In his survey of the Mediterranean, between Malta and
Crete +, Capt. Spratt afterwards found at the depth of 9720 ft. “nu-
merous dead shells and fragments of shells.”
The preliminary observations necessary before laying the dif-
ferent lines of Atlantic telegraphs next came in aid of natural
science. In 1855 a United-States steamer made a series of deep-
sea soundings across the Atlantic. The fine calcareous mud brought
up from depths of from 6000 to 12,000 ft. was examined by Prof.
Bailey, who discovered in it numerous shells of Globigerine and
Orbuline, with Diatoms and sponge-spicules. He doubted whe-
ther these Foraminifera could have lived on the sea-bottom, and
thought they might rather have fallen upon it from upper sea-zones-
* “Nature,’ vol. i. p. 166, Dec. 1869.
t Brit. Assoc. Reports for 1848, p.81. The depth given above is corrected on
Capt. Spratt’s authority. .
} ‘ Travels and Researches in Crete,’ vol. ii. p. 329.
e
xlvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Ehrenberg, on the other hand, believed that they had lived at those
depths.
Similar results were obtained on a line of still deeper soundings,
extending to 14,400 ft., made in 1857 by Capt. Dayman; and Prof.
Huxley, who reported on them, concluded that in all probability
the Globigerine did live at those depths.
In 1860 Dr. Wallich* carried out an important series of deep-sea
researches in connexion with the soundings made on board H.M.S.
‘ Bulldog,’ and obtained some very interesting results. He not only
confirmed the prevalence of a Globigerina-mud in the great depths of
the Atlantic, but also gave much evidence in favour of the Globigerina
living at those depths. Dr. Wallich also brought up two living
Crustacea from a depth of 2670 ft., and living Serpule, Spirorbes,
and Polyzoa from a depth of 4080 ft. His most remarkable dis-
covery, however, was that of living starfishes at a depth of 7560 ft.*
Dr. Wallich’s researches mark another epoch in the history of deep-
sea explorations.
The following year further discoveries were made in the Medi-
terranean, between Sardinia and Algiers}. It having become
necessary to raise the French telegraph cable after it had been sub-
merged five years, it was found that at places various Mollusca,
Corals, and Bryozoa had grown upon it. Portions of the cable,
stated to have been raised from depths of from 6500 to 9000 ft.,
were submitted to M. Milne-Edwards, who determined the following
species, to which I have added their geological range :—
Ostrea cochlear. Coralline Crag. Caryophyllia arcuata.
Pecten opercularis. Coralline and
electrica, sp. n.
Red Crag. Thalassiotrochus telegraphicus, sp. n.
—— Teste. Phi Salicornaria farciminoides.
Monodonta limbata. Sea ieels Serpula.
Fusus lamellosus. OMene Gorgonia.
The Swedish expedition to Spitzbergen in the same year (1861)
also determined the presence, at a depth of 8400 ft., of various
Mollusca, Crustacea, and Hydrozoa.
Between 1860 and 1868 a series of most valuable researches
was carried on off the coast of Upper Norway by the late Professor
Sars and his son, at depths of from 1800 to 2700 feet. At the former
depth they found an abundant fauna; at the latter the collections
* “Notes on the Presence of Animal Life at Vast Depths in the Sea,’
1860, and ‘On the North Atlantic Sea-bed,’ 1862.
t Ann. des Sciences Nat. 4¢ sér. vol. xv. p. 3.
ANNIVERSARY ADDRESS OF THE PRESIDENT. xvii
were smaller, but still considerable. JI annex a list of the number
of species dredged at the depth of 2700 feet, for the purpose of show-
ing how these researches already affected questions depending on
the relative proportion of recent and extinct species, as to the age
of the newer geological deposits :—
Known species. New species. Total.
IMIOUS Ca Ar scusearuessesiccsescor ane eneest 2 ae eA 11
@rustaceare een castece cacao eects ON pW yee ki tease oe 3
Hehinodermata ..........00....00+05 pres enero Ono tae. 3
Foraminifera ............s.ccesseesss DONS ae AT IN ENE As 24
32 9 41
In 1867 Count Pourtales* dredged, between Florida and Cuba,
in depths of about 3000 ft., and found a rich fauna of Mollusca,
Crustacea, Corals, and Echinoderms.
Impressed with the value of these observations, and with the
importance of a more systematic and yet deeper exploration of the
ocean-bed, Dr. Carpenter, at the suggestion of Prof. Wyville Thom-
son, brought the subject before the Royal Society in June 1868.
As the undertaking was beyond the reach of private enterprise, an
application was made by the President and Council of the Society.
to the Government for a vessel for the purpose. The request was
readily and liberally responded to; a Government steamer was then,
and again in 1869 and 1870, placed at the disposal of the Com-
mittee appointed for the purpose; and a most important series
of deep-sea dredgings haye been carried out by the above-named
naturalists and Mr. Gwyn Jeffreys. Only the general results have.
as yet been laid before the Royal Society. These, however, are
quite sufficient to show that the expeditions have proved of the
highest service to natural science, whether as regards the existence
and distribution of animal life at great depths of the ocean, the
temperature at various depths, the direction of the great oceanic
currents, or the bearing of such investigations on the past his-
tory of our globe.
Almost everywhere the deep bed of the Atlantic was found co-
vered in its greatest depth with a light-coloured calcareous mud,
abounding in Gilobigerine, rich in siliceous sponges, and often sup-
porting a varied fauna of Mollusca, Crustacea, and Echinoderms.
Numerous valuable observations were also made on deep-sea tem-
* * Bulletin of the Museum of Comp. Zoology,’ Cambridge, U. 8., 1867, and
‘Silliman’s Journal’ for Nov. 1868.
xlvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
peratures and currents, with instruments prepared for the occasion.
I must refer to the papers by Dr. Carpenter and his colleagues (to
whom I am much indebted for the perusal of the last Report, now
going through the press), in the ‘ Proceedings of the Royal So-
ciety’*, for the varied information respecting the composition
of sea-water at different depths, the gases contained in it, and the
speculations on oceanic currents. The points that more particularly
- interest us are those bearing on geological investigations.
In first drawing the attention of the Royal Society to the im-
portance of undertaking deep oceanic researches, Prof. Wyville
Thomson referred to the recent discovery by Prof. Sars of a small eri-
noid belonging to an order supposed to be extinct, and which flourished
from Jurassic to Cretaceous times ; he suggested the probability of
the continuity of the ancient chalk-sea with the present abyssal
depths of the Atlantic, as such depths would be but little affected by
any of the later oscillations of the earth’s crust in the northern hemi-
sphere, as, since the commencement of the Tertiary epoch, they pro-
bably had not much exceeded 1000 ft. The result of the first expe-
dition was more than sufficient to confirm the most sanguine antici-
pations. Dr. Carpenter, on its return, reported that, of the higher
types of marine animals which they had discovered, “ many carry us
back in a remarkable manner to the Cretaceous epoch ;” and, again,
it “‘ seems on general grounds highly probable that the deposit of Gilo-
bigerina-mud has been going on from the Cretaceous epoch to the
present time (as there is much reason to suppose that it did elsewhere
in anterior geological periods), this mud not being merely a chalk
formation, but a continuation of the chalk formation.” These views
have a high significance and interest. Let us see how far we can
adopt them. :
The Atlantic abyssal mud has been found to contain from 50
to 60 per cent. of carbonate of lime, 20 to 30 of silica, with small
variable proportions of alumina, magnesia, and oxide of iron. Its
appearance, when dry, is chalk-like ; but itis to be observed that our
white chalk is a much more homogeneous rock, containing from
95 to 99 per cent. of carbonate of lime, while even our grey chalk
contains from 80 to 90 per cent +. The larger proportion of cal-
* Proc. Roy. Soc. vol. xvii. pp. 168-200; vol. xviii. pp. 3897-492; and
vol. xix. pp. 146-222. ‘
t Since writing the above, Mr. David Forbes has kindly obliged me with the
following observations :—‘“ The specimens of Atlantic mud or soundings which
I have examined, differ very essentially from chalk in composition; and no
single one of them (if consolidated) could be entitled to the appellation of
ANNIVERSARY ADDRESS OF THE PRESIDENT, xlix
careous Foraminifera in the chalk, and of siliceous Polycystina and
vitreous Sponges in the Atlantic mud, may, however, render this
rather a question of proportion than of radical difference. I would
point out that the White Chalk (Terrain Sénonien) of Touraine varies
in colour from white to light yellow, or greyish yellow, is a much
less pure carbonate of lime, and is wonderfully rich in siliceous
sponges. In fact there is one portion of it, from 28 to 30 ft. thick,
which contains no carbonate of lime at all*. Atother places in
France, and in Europe, the chemical composition of the chalk
differs considerably, and the colour varies from white to dark grey.
Mr. Lonsdale +, many years since, pointed out that white chalk
was composed largely of microscopic organic débris, consisting chiefly
of minute Foraminifera; and Dr. Mantell+ afterwards estimated that
more than a million of such remains are contained in a cubic inch
of some of our chalk. I would further draw attention to a remark
by Dr. Mantell in the same work (p. 315). Speaking of the chalk,
chalk, as ordinarily understood by geologists or chemists. In order to make
a correct comparison of their composition with that of chalk, I was obliged to
make analyses of the latter rock, two of which I annex.
Grey Chalk White Chalk,
(base of), Shoreham
Folkstone. (Sussex).
Carbonate of lime <tr.cc-0.se--- sce se-eee 4 94-09 98°40
Carbonate of magnesia ..........0...-...268 031 0:08
Insoluble rock débris............000--.00-06- 361 1-10
IE WOSPHOLIC ACIOMeseetecsecerseeeesese esse traces
Alumina and loss in analysis ............ 5p | 0-42
Chloride of sodium .............0.-2-2e eee 1-29
WWWieteriiee: scakcwcticesse shee testaivecetcctmesscces 0-70
100-00 100-00
On the other hand, the specimens of Atlantic mud received from Mr. Gwyn
Jeffreys, Dr. Carpenter, and others (about eight in number), and examined by
me, contain at highest not 60 per cent. of carbonate of lime, along with very
much siliceous and aluminous matters, oxide of iron, &e.; and if we were even
to subtract the amount of water, organic matter, and marine salts found by
analysis in them, as these substances would be in greater part removed before
such mud could, in the process of ages, be converted into solid rock, the amount
of carbonate of lime would be stillefar less than that present in what would or-
dinarily be regarded as chalk; in fact the resulting rock would have the exact
composition of many of the older marls or impure limestones.”
* Mém. Soc. Géol. de France, sér. 1, vol. ii. p. 239.
+ Lyell, Anniv. Address Geol. Soc. for 1886, p. 13.
¢ Wonders of Geology, 6th edit. 1848, vol. 1. p. 805.
1 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
he says, ‘The whole forms such an assemblage of sedimentary de-
posits as would probably be presented to observation if a mass of
the bed of the Atlantic, 2000 ft. in thickness, were elevated above
the waters, and became dry land; the only essential difference
would be in the generic and specific characters of the imbedded
animal and vegetable remains.” Whether viewed by naturalists or
by geologists, the similarity of origin seems to have occurred to both;
and I am not aware that the question of depth ever seriously inter-
fered with this view amongst geologists, who, on the contrary,
rather considered the mass and fossils of the chalk to be an indica-
tion of the possibility of life at great depths. Both deposits were
also found to contain numerous peculiar and simple organisms, which
were named Coccoliths* and Coccospheres (noticed by Wallich,
Huxleyy, and Sorby), while the profusion of the particular Forami-
nifer the Globigerina, and the later discovery of siliceous Sponges,
are other features in common. Except by Mr. Bailey, the presence
of Diatoms has not been noticed +.
Prof. Rupert Jones has kindly filled up for me the following Tables,
the results being based chiefly on Messrs. Parker and Jones’s excel-
lent account of the Foraminifera from the North Atlantic and
Arctic oceans§. They determined 110 species as now living in
those seas; and of these they recognized 19 as fossil in the Chalk.
* Mr, Carter now considers this to be a calcareous unicellular alga, the frus-
tules of which form the Coccospheres. He proposes for it the name of Melobvesia
unicellularis. It occurs in abundance in the Laminarian zone off the Devonshire
coast. Another species, the M. discus, he considers peculiar to the deep Atlantic.
Ann. & Mag. Nat. Hist. for March 1871.
+ Prof. Huxley states that Dr. Gimbel of Vienna has now discovered these
bodies in all sedimentary strata.
¢ Count Ab. Castracane, of Rome, however, has since examined some of the
mud obtained in the first ‘ Porcupine’ expedition at a depth of 14,610 feet, for
Diatoms, and reports that he discovered a rare species of Asteromphalos, which he
found, for the first time in Europe, in the Adriatic in 1863. He states also
that “Specimens of Hemidiscus occur in greater number, and perhaps also
some allied species like Huodia, of which I am not aware that, up to the pre-
sent time, any examples have before been found in Europe; at least I have not
discovered any mention of them in the various authors I possess on the subject.
Besides these, the species of Diatoms most abundant in this deposit are the
Coscinodisci; and of these the Coscinodiscus lineatus, Khr., is the most fre-
quently met with. There are numerous Méelosire, Bacteriastra, Triceratia,
Bacillarie, Pleurosigmata, Synedre, Navicule,” &c. Count Castracane is unable
to determine whether these lived at the bottom of the ocean or near the surface.
(Accademia Pontificia de’ Nuovi Lincei, sess. del 8 Aprile 1870.)
§ Transactions of the Royal Society for 1865.
ANNIVERSARY ADDRESS OF THE PRESIDENT. li
Mr. Jones remarks that the numbers in the following Tables are
liable to modification with further research.
Other, older Formations in which
they are also found.
Speciest of Foraminifera found in both
the Atlantic mud and the Chalk of
‘England and Europe.
Upper
Jurassic
Lower
Jurassic.
Rheetic
and Trias.
Carbonife-
rous.
Glandulina levigata, D'Orbigny.| * | ....-
Nodosaria radicula, Linn.......... * *
raphanus, Linn. ..0...00002-| severe *
Dentalina communis, D’ Orb... Pensess * *
Cristellaria cultrata, ‘Mont. Hitesalt | 3e *
*
2
eoeeee | teveee
Subgenera
of the genus
Nodosarina,
TON, JOM Geegeceeeooseed| 45
crepidula, F’. f M... Balas
Lagena aoe WANG Seenuecaucnt nance ese
eecees | eaeeae | eaeere | soeees | eeesee
weeeee | ceseee | ceesee | cesses | teeeee
eaccee | sores | seeves
— communis, “"D Crisco ita Tics ata Neal dices lena hse. a aaa a
compressa, D’ Orb, .......ceseeeeeeeeees * * *
ODOM Peace verona odes taemale nel tusemertes (neeiecarall Manhie ce (lngeaeneyll: eeiraae
Globigerina bulloides, D’ Orb............2.0.) se...
Planorbulina lobatula, W. g J. ...........
Pulvinulina Micheliana, D’ Ord.............
Spiroplecta biformis, P. g J. ...| ......
eeeeee | eoeves | eoceee | eevee
Verneuilina triquetra, v. M.......| ......
polystropha, Rss. ..........0.) cecee. | cee eee
ES
~
s
~
oH
Bupoeuers
laria,
°
eeecee | eveces | ceeeee
Besides the above, Bulimina (Bolivina) punctata, D’Orb., is found
in the Atlantic mud and in the Upper Jurassic, and Nodosarina
(Dentalina) pauperata, D’Orb., occurs in the Atlantic mud as well as
in the Lower Jurassic and the Upper Trias.
Number of Species of Foraminifera common to the Atlantic Mud and
to the several undermentioned Geological Formations in England.
Common to the following Formations.
Total in
the deep Thaudow U Rhetic & : Carbo-
: pper | Lower Permian] <p
ettlamne-| Crag. Clay. Cini Jurassic. | Jurassic. me ae strata. es
110 53t 28§ 19 7|| 7|| 7 ] 1
t Accepted species and noticeable varieties.
{+ There are 12 other species in more recent beds.
§ The total in the Lower Tertiaries is 36.
|| Common to both Upper and Lower Jurassic, 9.
li PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
With the Foraminifera, however, end the specific identities be-
tween the Chalk and the Atlantic mud. Beyond this group we find
resemblances or affinities only. Siliceous sponges, of which no less
than 20 genera have been dredged, abound, it is true, as they do in
the Chalk; but they are either new forms, or are Mediterranean
and Azorean species. Professor Thomson* remarks that the Ven-
triculites of the Chalk are represented by the group of Porifera Vitrea, —
that the species of Sympagella, Holtenia (Spheroma), and Farrea
approach the Siphonias and Ventriculites very nearly, but that they
form a distinct subsection of the order. Echinoderms abound, as in
the Chalk; and species of the genus Cidaris are numerous, while
some forms of Diademide approach the curious Hchinothuria of the.
Chalk. The “Saleniz, Cassidulide, and Dysasters approach their Cre-
taceous antetypes more closely than any known forms; but they are’
generally dwarfed, and otherwise diverge so far as to require in most
cases the establishment of new genera for their accommodation.” :
The Bowrgueticrinus of the Chalk is represented by the beautiful
Rhizocrinus, first found by Sars off the coast of Norway, and after- _
wards by the ‘ Porcupine’ expedition in the North Atlantic; and the:
Brachiopoda are represented by the smooth forms of Yerebratula so
common in the Chalk; while the 7. ( Waldheimia) cranium may be
considered a Chalk type.
Dr. Carpenter further remarks upon the occurrence of numerous
arenaceous forms of Foraminifera analogous to the gigantic forms
discovered in the Upper Greensand by Prof. Morris; and there is
one that can certainly be identified with a form lately discovered
by Mr. Brady in a clay-bed of the Carboniferous Limestone t. The
presence of the Xanthidia, so frequently preserved in chalk flints,
is also observed in the Atlantic mud. Some southern forms of star-
fishes are found. dwarfed from a diameter of 6 inches to one of
2 inches, together with a number of Kchinoderms previously known
only as Norwegian or Arctic. On the other hand the Foraminifera
are large, asin warm climates or in Tertiary beds, or as with the Cris-
tellarian and Milioline groups. Amongst fishes a Beryx was found,
a genus of which there are 4 species in the English Chalk.
It is also to be noticed that we have in the Chalk the first repre-
sentatives of the cycloid fishes, which have their maximum develop-
ment in existing seas, and that, of the 103 genera of testaceous
* « Nature’ for July 1870.
t It was in beds of this age that Prof. Phillips, some time since, indicated the
presence of Globigerina.
ANNIVERSARY ADDRESS OF THE PRESIDENT. hii
Mollusca found in the Chalk, 80 (of which 19 make their first
appearance at that period) are living at the present day. At the
same time it is not in the deep Atlantic, but rather on its warmer
coasts, that we now find the widest dispersion of this group of cre-
taceous genera.
These constitute the main points of resemblance. Striking as they
are, their limits are confined ; and, on the other hand, the divergences
are great. The great feature of the Chalk-fauna is the abundance of
Cephalopods and its large reptiles, so very few genera of which have
descended to present times. The relative distribution of genera of
the principal Invertebrata was, according to D’Orbigny*, before the
late discoveries, approximately as under :—
Number of genera.
eT
—
In the I Extinct vie
White Chalk. with the Chalk. 8:
Cephalopods .................. Saal pareebnse MATa rsitocls 1
Gasteropods .................. ATi Oieseas SU ance 32
Lamellibranchs ............... BPA Lie ace 41
Brachiopods .......0........+. HO eeshao Supers eases 7
Echinoderms ...............06 SAE Peach DT cose 7
150 62 88
With the Cretaceous series disappear the many genera of Cephalo-
pods allied to Ammonites which range through the Triassic and
Jurassic formations, together with the Rudistes, so peculiar to the
Chalk period.
The Mottusca of the deep Atlantic are still undergoing investi-
gation at the hands of Mr. Gwyn Jeffreys. Enough, however, is
already known of the remarkable results to form some opinion of
its great value in a geological point of view. The total number now
dredged may probably exceed 300 species. Of these, 86 species
have been recognized and are noticed in the Reports now published.
A very large number are altogether new. With the aid of Mr.
Jeffreys, I have drawn up the following lists, which will serve to
show the light which may be thrown on the paleontology of our
more recent Tertiary strata by these inquiries. Of the 86 deter-
mined species, 67 were known before as living, though chiefly as
high Northern and Arctic species (while the wider range of some
few of the species is very remarkable), and 19 are fossil species
* Paléontologie et Géologie stratigraphiques, vol. iui. § Terrain Sénonien.
liv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
previously supposed to be extinct. Of the 67 known living species,
there are :—
Species living in the North Atlantic and Arctic seas ...... 51
Species living in the Mediterranean .................0:.ce000e- 11
Species living in the Gulf of Mexico...........-.c:.cceeeeeeee 2
Species living in the Japanese seas .........s.ccseeceeeeneeees 3
67
Among these 67 species, 45 were known as fossil also in the
Pliocene beds of Italy and Sicily or in our Crag.
Fossil in Italy and Sicily............... 25
Fossil in the Crag.................00+ vee. 20
45
Of the 19 species which had hitherto been known only in a fossil
state, I give, with Mr. Jeffreys’s assistance, the list in full, for the
purpose of showing their geological range and position.
List of Mollusca known hitherto as Fossil only, and now discovered to
be living in the depths of the Atlantic.
Depths dredged *. Species. Locality where found fossil.
feet.
1932 to 2184. Cancellaria mitrzeformis. Italy and Coralline Crag.
1932 to 2184. subangulosa. Coralline Crag.
5694. Cylichna ovata. Sicily and Coralline Crag.
1542 to 4140. Leda obtusa. Sicily and Calabria.
4308. pusio. Calabria.
1752 to 2244, Limopsis minuta. Sicily.
4308. pygmea. Sicily.
1680 to 1824. Odostomia plicatula. Italy.
3600 to 6570. Omphalius monocingulatus. Sicily.
1542 to 4140. Pleurotoma decussata. Calabria, Sicily, and Coral-
line Crag.
4140. Rhynchonella sicula. Sicily.
1542 to 4140. Rissoa subsoluta. Sicily and Calabria.
3600 to 6570. Scalaria frondosa. Italy and Coralline Crag.
3600 to 6570. Siphonodentalium coarctatum. Italy.
3600 to 6570. Trachysma delicatum. Sicily.
1680 to 1824. Trochus crispulus. Sicily.
1542 to 4140. reticulatus. Sicily and Calabria.
2148 to 4302. suturalis. Sicily and Calabria.
3402. Turbo filosus. Calabria.
* Other species of mollusca continued to be dredged down to depths of
14610 feet.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lv
Mr. Jeffreys informs me that, in addition to the above, there are
many other species in the same category, though they have not
yet been specially recorded. According to him, the total number
of species which were, until lately, considered extinct, but which
he has now ascertained to be living, is at least thirty.
In the Mediterranean, there is at present little to record. 15
species were dredged from a depth of 8490 feet. They consisted
of :—
Northern Species......c0.cce:ssces 5 | Fossil in Italy ..........0000. 69)
MiASTUATI A een ated csuieeisy eee 9 | Fossil in the Crag ........ ...+4 4
QEMMNG ooccoaoqoecooesasosoonecnoD iy Newaspeciest te-ssiecameenese cree 2
Some new species of much interest were discovered in less depths (of
from 100 to 1000 feet) in and at the entrance of the Mediterranean.
Amongst these there were 31 northern species, also 12 species
before known only as fossil in Italy, and 3 species common to our
Crag.
Thus, so far from showing any relationship to the Cretaceous fauna,
the deep Atlantic mollusca have their nearest allies in Pliocene
(and possibly Upper Miocene) forms of Italy and in those of the
Crag-beds of this country. Mr. Jeffreys’s anticipations, made in
1862 *, that “it is highly probable that all the mollusca which
lived during the periods represented by the newer strata still sur-
vive in some part or other of those vast tracts of sea-bed which lie
between the North Pole and the Pillars of Hercules,” and that the
deeper recesses of the ocean would be found inhabited, receive
therefore great confirmation, though it yet remains to be seen to
what extent they may be fully realized. Almost all the species yet
found at these great depths are, like so many of our Coralline-crag
species, very small.
Prof. Duncan has described + 12 species of corals dredged from
depths of from 2000 to 4200 feet; and he informs me that he has
under description many others, some of which were obtained from
a depth of 6570 feet. Owing to the great range in depth and -
temperature of the Atlantic sea-bed, the variation in form of some
of the corals has been so excessive that Prof. Duncan has absorbed
9 old species in the 12 now established. The range and distribution
of these species thus obtained in the first and second expeditions is
very remarkable.
* ‘British Conchology,’ Jeffreys, vol. i. p. xci.
t Proc. Roy. Soe. vol. xviii. p. 289.
lvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Allopora oculina, Zhren.—Original locality unknown.
Caryophyllia cyathus, Hillis g Sol. sp.—British Seas,
Mediterranean. |
Lophohelia prolifera, Pallas.—British Seas, Mediterranean, bt Sletten
Pipeida Seas 4 Older Pliocene.
Flabellum laciniatum, Hd. § H.—British Seas.
Ceratocyathus ornatus, Seg.—Fossil. |
Amphihelia miocenica, Seg.—Fossil.
atlantica, Dunc. New.
oculata, Linn. sp.—Mediterranean.
ornata, Dune. New.
profunda, Powrt. New.—West-Indian Seas, Mediterranean and Nor-
wegian Seas.
Balanophyllia socialis, Pourt. New.
Pliobothrus symmetricus, Pourt. New.
\ Florida Seas.
Thus out of 12 species there are as many as 5 which were before
known as fossil only ; or if we take the annulled species, there were
8, all of which had hitherto been confined to the newer Tertiary beds
of Sicily or southern Italy. Unlike the Testacea, which show a rela-
tionship to northern forms and to those of our Crag, there is not a
single species that Prof. Duncan has been able to refer to the Crag,
whilst the connexion with the Mediterranean area and with the seas
of Florida and the West Indies is most noticeable. Prof. Duncan
regards one or two of the new species as allied to Miocene forms;
but he does not instance a single case of an approach to Cretaceous
forms, except possibly in the case of Lophohelia (to the Synhelia of
the Chalk) and Diplohelia, which is really an Amphihelia.
Among the Corals, however, now under examination from the
second expedition of the ‘ Porcupine’ the Sphenotrochus of the Crag
is found (locality Tangier Bay), and some Caryophyllie and Bathy-
cyathi of Cretaceous types are to be noticed.
Thus while the Foraminifera obtained in these deep-sea explora-
tions show a strong community of genera and a partial identity of
species with chalk Foraminifera, the Sponges markedly representa-
tive forms, the Echinoderms allied genera, and the Brachiopoda
a similarity of groups, on the other hand, as we ascend in the scale,
so far from any resemblance being maintained, we find actual iden-
tities with the Upper Miocene*, Pliocene, and Quaternary fauna of
western Europe. This seems to point to a possible direct descent in
the one case of all those lower forms of life, less influenced by
temperature and depth, from the epoch of our chalk, and in the
other case to a change of physical conditions, resulting from the
* There is nothing which has the facies of the Eocene Molluscan fauna.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lvil
different arrangement of our seas and continents, destructive of the
higher forms of life, and accompanied by the introduction of northern
forms of partly corresponding classes.
Edward Forbes concluded from his researches in the A‘gean that
parallels in latitude are equivalent to regions in depth ; and he subse-
quently showed this hypothesis to hold good by the occurrence at
various depths in southern seas of northern species of mollusca. Hence
cold-water species of Testacea can have a much wider range in
latitude than warm-water species. MM. D’Archiac and De Ver-
neuil had already, on purely paleontological grounds, concluded
that those species which were found at many places, and in districts
distant one from the other, are almost always those which have lived
through many successive formations (systémes)*; or, as it was better
expressed by Mr. Rogers, “ the species of which the geographical castri-
bution is the widest have also the greatest vertical range.” Reasoning
from these data, M. D’Archiac observed that those geologists who
saw “beds of different age everywhere where they found different
fossils, were liable to make serious mistakes ; for the same bed taken
at two distant points and haying a natural difference of level, say
of 300 feet, might present very distinct groups of species, and might
lead to the erroneous conclusion that these two parts of the same
bed were not contemporaneous ”’>. Edward Forbes also observed
* Bull. Soc. Géol. de France, vol. xiii. p. 260, 1842.
+ Bull. Soc. Géol. de France, 2nd ser. vol. ii. p. 484, 1845. As the discussion
which ensued on this communication bears on the subject of these deep-sea
investigations, I give a few extracts from it, which may be new to some present :—
“M. de Verneuil ajoute que, sur les cotes de Suéde et de Norvége, 1a ot la
mer est assez profonde, M. le Professeur Lovén, de Stockholm, a observé parmi
les mollusques une distribution verticale correspondant a leur distribution hori-
zontale, suivant les latitudes. Ainsi, entre Gothenbourg et la Norvége, M. Lovén
a trouvé 4 80 toises de profondeur, des espéces qui, sur la cote du Finmark,
habitent a 20 toises; plusieurs espéces s’élévent méme sur cette derniére céte
jusqu’a la région littorale, tandis que dans le sd elles se tiennent toujours a
12 ou 15 toises au-dessous du niveau de la mer.’
“MM. Elie de Beaumont fait remarquer... . Anjourdhai: la température a la
surface de la mera l’équateur est de 274° [C.], tandis qu’au fond elle est de 2°. Tl
n’y a aucune raison de croire 4 ces différences autrefois.” .... “La trés-grande
masse de la mer équatoriale est 4 une température trés-basse et seulement d’un
petit nombre de degrés au-dessus de zéro.” ™
M. Pouillet also, in his ‘Hléments de Physique,’ vol. i. p. 166, 1847, speaking
of deep-sea fishes, observes: “On peut juger par la que les régions dela mer ont
leurs peuples différents, non seulement suivant les climats, mais encore suivant
les profondeurs.”
VOL. XXVII. é
lvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
‘that all climatal inferences drawn from the number of northern
forms in strata containing assemblages of organic remains are
fallacious, unless the element of depth be taken into considera-
tion ” *,
I mention these observations (made many years since, and which
of late have generally been taken into account in all geological
inquiries) to show that geologists have still to be guided by the
same primary natural-history rules, which have lately received
so wide an extension and application in these recent deep-sea
dredgings.
The mistake made by Edward Forbes was his assigning the
too narrow limit of 1800 feet in vertical depth as the probable zero
of animal life in the ocean. Dr. Wallich afterwards extended the
probable limits of life to 15000 feet; and now the important re-
searches of Carpenter, Jeffreys, and Thomson show that it must in
all probability be carried very much lower, as they have found a
highly organized fauna living in abundance at the vast depth of
14,610 feet, and no indication of an approach to the zero of life.
It had, in fact, been long felt that the proposition involved in these
bathymetrical limits was open to question.
The many interesting problems connected with the temperature
and currents of the ocean have often engaged attention since the
early part of this century. It was one of the subjects respecting
which a large amount of data was collected on the several scientific
naval expeditions sent out by the French Government between 1820
and 1840. Humboldt states} that he showed in 1812 that the
low temperature of the tropical seas at great depths could only be
owing to currents from the poles to the equator.
D’Aubuisson, in 1819, also attributed the low temperature of the
sea at great depths at or near the equator tothe flow of currents from
the poles ¢.
Lenz §, in 1831, gave the results of some experiments he had
made at great depths in the ocean, and concluded that between the
equator and 45° of lat. the temperature decreases regularly to the
depth of 6000 feet, when the decrease becomes insensible. The
lowest temperature he recorded was 36° Fahr.
* Edinb. New Phil. Journ., April 1844.
+ Fragmens de Géol. et de Climatol. Asiat. 1831.
+ Traité de Géognosie, p. 450.
§ Edinb. Journ. of Science, vol. vi. p. 341.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lix
Pouillet * briefly discusses ocean temperatures, and concludes
that, although all the difficulties of the case are not solved, it seems
certain that there is generally an upper current carrying the
warm tropical waters towards the polar seas, and an undercurrent
carrying the cold waters of the arctic regions from the poles to the
equator.
The early evidence on the subject was necessarily contradictory, as
the instruments were often imperfect, and the temperature in the
early experiments was often taken by means of water or mud
brought to the surface. Off the coast of Greenland, Scoresby al-
ways found the temperature in descending to increase, in some
cases, to 36° or 38° F., while the surface-temperature was only from
28° to 30°. He mentions, however, that in lat. 72° 7'N., long.
19° 11' W., where the temperature was 34° F. at the surface, it was
29° at a depth of 700 feet. Sir Edward Parry found the surface-tem-
. perature off Spitzbergen to vary from 28° to 31°, and at depths of
from 400 to 600 feet to be from 30° to 28°. Sir John Ross found the
temperature at a depth of 2520 feet in Melville Bay to be 293°;
in Lancaster Sound, depth 7900 feet, 29°; and in lat. 72° 33' N.
and long. 73°'7’ W. the surface-temperature was found to be 35°,
decreasing gradually to 282° at a depth of 6000 feet. More lately
the carefully made observations of M. Chas. Martins in the Spitz-
bergen seas led him to the following conclusions :—
ist. In the months of July and August the temperature of the
surface, although near freezing-point, is always somewhat,
above it,
2nd. From the surface to a depth of 240 feet, the temperature
here increases, there decreases.
drd. From 240 feet to the bottom the temperature always de-
creases.
4th. The mean temperature of the water at the bottom of the
sea is 28°84° F. (— 1:75° C.).
The greatest depths of the soundings seem to have been from 2000
to 2800 feet.
These low deep-sea temperatures have not only been found to pre-
vail in high northern latitudes, but to extend, though in some-
what diminished force, to the equator, and thence to the Antarctic
regions.
* Hlém. de Phys. vol. ii. p. 667, 1847.
e2
lx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
The following instances, taken from the many made on different
voyages of discovery, will suffice to illustrate this fact :—
Temperatures of the Atlantic.
Longitude Temperature.
Latitude. (corrected Depth. .—-—_~———. Observer & Date.
to Greenwich). Surface. Bottom.
ths Ct a ft.
42 ON. 3440W. 4688 620 4405. Chevalier 1837.
29 ON. 34 50 W. 8399 760 43:0 ” ”
721 N. 20 40 W. 3030 80:0 36:0 Lenz 1832.
425N. 26 6 6037 80:8 379 Tessan 1841.
15 38. 23 14 W. 7200 770 39:5 ” »
25 10S. 7 59H. 5315 674 376 1 »
29 338. 10 57 BH. 6310 66-4 358 % 7
32 208. 43 50 H. 6444 710 36:5 Lenz 1832.
38 128. 54 80 W. 2000? 624 376 Tessan 1841.
In the Antarctic regions Sir James Ross made a considerable
number of observations in 1839-43. Whatever the temperature of
the surface, he found the temperature from 2800 to 3600 feet to
be from 88° to 39-8°, the higher temperature being at the lower
depth. He concluded that below 1800 feet there was very little
variation in temperature, and inferred that in lat. 56° 14'S. there —
is an ocean belt, the temperature of which from top to bottom is of
39°5°. This conclusion seems to have been based on an erroneous
idea of the specific gravity of sea-water, and is possibly in some
degree attributable to errors of the instruments used. Captain
Willis, however, came to the same conclusion with respect to a belt
of uniform temperature. I cannot find that there is any sufficient
foundation for this hypothesis, which is in no way confirmed by the
observations of others. As the other observations were not generally
known, this hypothesis has unfortunately been too often accepted.
Later experience has shown that in many instances there is an
error in the earlier observations, in consequence (where proper
precautions were not used) of the pressure on the thermometer at
great depths. Dr. Carpenter has determined this to amount to as
much as 2° or 3°, or even more. Consequently a deduction to this
extent has often to be made in order to get a true reading of some
of the older observations. In many of the French expeditions,
however, great care was taken to guard against the influence of
pressure.
If we turn to the Pacific, we shall find similar low temperatures
prevailing at great depths both in the temperate and torrid zone. I
again take merely a few cases in illustration.
ANNIVERSARY ADDRESS OF THE PRESIDENT. ]xi
Temperatures of the Pacific.
Longitude Temperature.
Latitude. (corrected Depth. Observer & Date.
to Greenwich). Surface. Bottom.
fo) ‘ fo) Z ft. fe}
51 34N. 16141 EB. 5741 532 366 Tessan 1832
28 52N. 173 OF. 3600 780 41:0 Beechy 1828
18 5N. 174 10E. 4261 766 408 1836
432N. 134 24W. 12271 81:0 35:2 The ‘Bonite’ 1837
Equator (near) 179 34 W. 6000 860 366 Kotzebue 1824
21 148.
196 1W. 5500 810 3860 Lenz 1834
32 57S. 176 42 E. 4692 614 41:8
43 478. 80 6W. 6400 556 362 Tessan 1841
These observations tend to show that in the greatest depths, both
of the Atlantic and Pacific Oceans, the temperature is not higher
than from about 36° to 40°; and allowing for correction of the in-
struments, the actual temperature will probably be found to be in
many cases 2° or 3° or more below this. A more systematic mode
of proceeding, however, is needed ; for though the general rule may be
considered to be established, local variations and exact measurements
have to be ascertained. Notwithstanding, less attention has been
paid to the subject of late years than formerly. Dr. Carpenter has
now taken up the investigation, and has during the last three
years carried out a series of observations in the North Atlantic
which must prove of high value. Every care has been taken to
guard against error; and we shall soon no doubt have tables of
temperature at all depths in this part of the ocean, which it is
to be hoped will, concomitantly with the dredging-operations, be
extended over the whole of the oceanic area.
Time will not allow me to enter upon the question of the course
and cause of the cold under-stratum of the great oceans. As before
observed it has been generally referred to undercurrents from the
poles; and later observations tend to confirm this; but whether
in the mid-Atlantic the flow is from the north or the south pole
remains to be decided by more accurate inquiries. My own opinion
inclines to an undercurrent from the North Pole. The occurrence
of boreal and Scandinavian forms of life far south in the Atlantic
favours this view. Whatever the cause, the fact of cold under-
currents, which must have a powerful effect in bringing northern and
southern forms into close vertical juxtaposition, is indisputable. All
seas open to the Arctic and Antarctic oceans are doubtless subject to
these conditions of warm surface-currents from the equator and cold
undercurrents from the poles. In seas where there is no direct
Ixii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
communication with the Polar seas, the case must assume a very
different aspect.
Dr. Carpenter in his last cruise made also a number of observa-
tions in the Mediterranean, showing that while the surface-tempe-
rature in August and September varied from 69°5° to 77°, it fell
in all cases to about 56° at a depth of 600 feet, and maintained
that temperature through all the depths below thatline. This con-
firms the experiments made in 1840-1845* by M. Aimé, who found
that the average temperature of the sea at a distance from land, for
the twelve months of the year, was 64-4° Fahr., that of the air
being 64:8°; and that the former decreased gradually to 54°6° at
a depth of 1148 feet, below which to a depth of 4050 feet it was
not found to vary 1°+. He considered that the diurnal variation
of temperature ceased at 59 feet, and the annual variation at from
1148 to 1640 feet, although, in fact, his tables show little variation
after 656 feet. The mean shore-temperature of January, February,
and March, taking together the two stations of Toulon and Algiers,
was ascertained to be 54:8°, with which the temperature of this part
of the depths of the Mediterranean corresponds almost exactly.
The subject of the currents and temperatures of the Mediterranean
engaged also the attention of Captain Spratt for a series of years,
and a number of carefully made experiments are recorded by him.
He also determined that while the temperature from the surface
to a depth of 12 feet ranges generally from 76° to 84° Fahr.,
gradually decreasing to a-depth of 600 feet, there was little va-
riation below that line, and that the temperature of the depths of
the eastern basin of that sea is about 59°, and of deep seas off Greece
554°—that while on the Mediterranean side of the Straits of
Gibraltar there is a deep-sea temperature of 59°, there is one of
394° on the Atlantic side t.
* Ann. de Chimie et de Physique, 3rd ser. vol. xv. 1845.
t The following is M. Aimé’s summary :—
‘‘ Températures moyennes annuelles de la mer a diverses profondeurs.
Températures. Maxima des variations entre
— —A— —— les moyennes mensuelles.
& la surface ...............065 1 Role? ean OS Maney mau aes aBeGna 10:2° C.
By 25 METRES ue sesawoulwsic sail Orsiy lun memunaecuaceccese 6:3
BHO OM ged Rep ee ea ar irate A i ee st ee aabe weiss 28
a LOO VE a amen ieaceoter Sid, mon ener ataasccceseae 2-0
ZOO Eee Sealer DS Oe aioe te aaa 1-0
Bc BOO) (is Ve ee es CNS ZG Ne AR SER Ty 0:0”
{ British Assoc. Report (Sections), 1848; and ‘ Travels in Crete,’ vol. ii. p. 345.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lxiil
The fauna of the Mediterranean naturally presents a consi-
derable difference from that of the Atlantic, especially from that
portion which inhabits the greater depths of the latter. There is
an absence of the numerous recent arctic forms which follow the
cold currents of the Atlantic, although there are many northern
forms of Quaternary and Pliocene age, which seem to have been
introduced into the Mediterranean area at a period when the com-
munication between the two seas may have been more open—an
‘inference made by several observers both on natural-history and
on geological grounds. Newer Tertiary strata extend, in fact, a
great part of the way across from the Bay of Biscay to the Medi-
terranean, and the watershed between the two seas is not higher
than about 600 feet above their levels. At one point on this line,
and at an elevation of 560 feet above the Mediterranean, M. Virlet
d’Aoust many years since discovered, in a fossil state, the Ostrea
hippopus and Murex trunculus, species still living in that sea.
From these considerations the question arises whether the deep
sea in which the Chalk, with its more tropical genera, was de-
posited, may not also have been a sea shut out from direct com-
munication with Arctic seas. The Old and New continents have
a north and south extension, with intervening oceans in the same
direction ; but the distribution of land and water must have been
very different during the Cretaceous period. Beds of this age stretch
from England through France, Germany, Poland and Southern
Russia to Persia and India, and they also traverse the southern
portions of the North-American continent. Throughout much of
Kurope and parts of Asia the Chalk has the common character that
it possesses in England, and which has led it to be likened to the
Atlantic deep-sea mud. On the other hand, there is no Chalk north
of Denmark, in North Russia or Siberia, or in Arctic America. If
the direction of the deep Chalk-ocean followed this east and west
belt across the present continents, then we must look for dry land
on the confines of that ocean; and it is probable that the latter
may have been, to the north, in the direction between Greenland
‘and Scotland and Scandinavia, where the present ocean is some
hundreds of fathoms shallower than further south. We know
that towards the end of the Cretaceous period, a change took
place in the fauna, arising apparently from the shallowing of the
sea that preceded the deposition of the Maestricht beds, as well as
of the Calcaire pisolitique of Laversine and Mont Aimé. Many
of the great Cephalopods disappeared, and reptiles increased in
lxiy PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
numbers ; at the same time the Lamellibranchiate Mollusca became
more predominant. Dry land appeared further south, as evinced
by the lignite and freshwater beds intercalated in the Cretaceous
series of Southern France. At the close of this period the con-
tinent of Europe may have acquired larger dimensions, although it
was not until after the great Nummulitic sea of Lower Hocene age
(which also stretches through southern Europe to India) had become
in part dry land that the “relief” of the continent approximated
to that of the present day. On the western edge of the new land
formed by the elevation of a portion of the old Chalk ocean more
littoral deposits then began to form ; and the same thing took place
on the sea-belt of the American continent.
The Cretaceous formation of the south-west of England and west
of France and north of Ireland passes out under the Atlantic, and
reappears on the south-east coast of the North-American continent.
As it thus trends in the same direction on both sides of the At-
lantic, there would be nothing improbable in supposing that old
Cretaceous ocean prolonged further in the same given direction
across the present Atlantic.
It is well known that at a distance varying from 50 to 200 miles
off the coasts of western Europe, the sea-bed deepens rapidly to 600,
then to 1200 feet, and again almost suddenly to depths of from 6000
to 15,000 feet. Does this mark a boundary of the materials drifted out
to sea during Postcretaceous times? or is it a line of still older date ?
The great and distinctive feature of: the Tertiary series is that,
with few exceptions, the whole of them were deposited in shallow
seas. ‘The London Clay even, which is from 400 to 500 feet thick,
does not represent a sea-bed deep in proportion, as there is eyi-
dence to show that it was probably deposited during a period of
gradual depression of the sea-bed. The total thickness of all the
English Tertiaries does not exceed 2000 feet, or that of the Paris-
basin Tertiaries 1500 feet *. Therefore, while the deep Atlantic
area continued submerged, movements of elevation and depression
affecting the continental European area (leaving out the changes
during the Glacial period) may have gone on during the Tertiary
period to the extent of from 2000 to 5000 feet, leaving abyssal
depths of from 10,000 to 12,000 feet unaffected by these move-
ments, even supposing they extended over the oceanic as well as
the continental area. It is the same on the American coast of
* Though further south the Tertiary beds attain possibly a thickness of from
3000 ‘to 4000 feet.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lxv
the States, which is bordered by Tertiary strata of a like character
with their European equivalents.
It is true there have been elevations of the Cretaceous and
Tertiary strata during the Tertiary period far greater than the
depths first mentioned; but it has been in mountain-chains which
have little affected the great plains of continental land. In the
same way there may have been partial elevations in the bed of
the Posteretaceous Atlantic ; but there is nothing to indicate that
it has ever been entirely raised. I think, therefore, that the hypo-
thesis with regard to the continuity of that sea-bed from the period
of the Chalk to the present period is one of high probability.
If such a northern land barrier as that which I have alluded to
existed at the period of the Chalk, and that barrier was submerged
during the early part of the Tertiary period, it would (taken in con-
junction with the very different conditions of depth under which
the Chalk and Lower Tertiaries were formed) go far to account for
the great break in the fauna of the two periods. Some years since
{ had oceasion to show on other grounds that the Thanet Sands,
which repose on the Chalk in the south-east of England, exhibited
a fauna essentially of temperate or cold latitudes, and I inferred
the inset of currents from the north. As those remarks bear upon
the present question, I will quote some of the passages in the paper
to which I refer *.
‘In viewing the London Tertiaries as a group, and comparing
them directly with the underlying Chalk, it is to be observed that
we are not comparing like terms of the two periods. That a great
and essential difference existed between these periods must be ad-
mitted; but it is a question. how far that difference is widened by
the comparison being instituted between the deep and shallow sea
deposits, instead of between strata deposited under like conditions
during those two periods. .... The adaptation of this area at the
Thanet-Sands period to the existence of the numerous shallow-
water burrowing Lamellibranchiates, whatever the duration of the
intervening time, would necessarily unfit it for the deeper-sea
Cephalopoda, Brachiopoda, and other families which prevail in our
Cretaceous series.
«‘We have therefore, in viewing the Tertiary strata in relation
to the underlying Chalk, to take into consideration that the exist-
ence of certain classes of fossils in the former of necessity implies
the non-existence of other classes found in the latter deposit—and
* Quart. Journ. Geol. Soc. vol. x. p. 443, Nov. 1854.
lxvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
this, even should the two have been in consecutive aud uninter-
rupted sequence in time.
“The somewhat Cretaceous facies which exists, however, in the
Lower Landenian [of Belgium] and the Thanet-Sands fossils, is
to be recognized in some portion of the fauna of the London Clay
itself. Thus among the Echinodermata the Hemiaster, a common
Cretaceous genus, has three species in the London Clay, and but one
in the Barton Clay ; whilst the prevalence of Crinoids, amongst which
is a species of Bourgueticrinus, hitherto considered a Chalk-genus,and
three species of Pentacrinus, and the new Cainocrinus of Forbes,
are features more resembling those prevailing in Mesozoic than
those usual in Tertiary strata. The two genera of Asteride (Astro-
pecten and Goniaster) which occur in the London Clay are common
in the Cretaceous strata, the Oolites, and Lias.”
‘The London Tertiary group seems to have resulted in that order
of changes which, commencing with the elevation of a portion of the
Chalk area at the end of the Maestricht period, was followed by sub-
sequent depressions which led to the transgressive accumulation of
the Lower Tertiaries from north to south...... I have before
shown the probability of the existence of dry land to the south and
an open sea to the north during the Thanet-Sands period, and of
more insular conditions during the Woolwich and Reading series
period ; and now with respect to the London Clay the evidence tends
in the same direction.”
“To have just terms of comparison, we need a Cretaceous series
with a similar varied marine, estuarine, and fluviatile fauna, such as
flourished during the successive Tertiary periods. We have already
in the Maestricht beds a change in the fauna—a dying-out of many
old forms, and the appearance of many genera common in the Ter-
tiary series.”
«In considering all these singular vicissitudes, and in contem-
plating the extent to which certain more northern influences ope-
rated in giving to a large portion of the fauna of the London Terti-
aries an aspect much more closely resembling that of the present
day than is found to exist in many more recent deposits, the
question suggests itself of how far that law, enunciated by Prof.
E. Forbes, and according to which the distribution of Molluscs in
depths of southern seas is equivalent to their appearance at lesser
depths or at the surface in parallels of latitude of more northern
seas, may by analogy be applied geologically in accounting for any
abnormal condition in the vertical succession of organic remains
ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixvii
such as here occurs? Can it be that such a group of generic forms,
allied to and closely resembling those found in the same zoological pro-
vince at the present day, had a yet older existence in more northern
proyinces—that generic forms of temperate regions have travelled
- from the north, and have been gradually spread further south,
giving, when they encroached upon the more southern forms, a more
recent aspect to the faunas of such various geological periods than
prevailed in those of the same localities when changes in the distri-
bution of land and water brought back for a time the southern forms
which had been temporarily displaced ? ”
That much of the difference between the fauna of the Chalk and
the Lower Tertiaries must be due to the elevation of the old Chalk
ocean-bed (by which the deep-sea life was exterminated and a shal-
lower-water fauna introduced) is now evident from the recent deep-
sea dredgings. Suppose, for instance, a portion of the present bed
of the Atlantic were raised to the level of the sea~bed of the present
English channel, whereby the depth of water would be reduced
from 12,000 or 15,000 to 100 or 600 feet. The deep-sea fauna
would be destroyed, and the fauna and sandy beds of the English
coast would succeed it; and when these were raised, we should
have sand and gravelly beds containing a shallow-water fauna
overlying calcareous beds with a deep-sea fauna, and there would
be but very few, if any, species common to the two deposits.
As old coast-lines and the oceanic currents changed during the
Tertiary periods, we may suppose corresponding changes in the fauna
of the littoral and laminarian zones, while thedeeper-sea fauna (which
was not subject to these changes of conditions) may have had a much
longer and more permanent existence. Together with the recurring
bathymetrical conditions, the lithological character of the sea-bed
further influenced the vitality and persistence of species. The Mol-
lusca of the Calcaire grossier of the Paris basin are, according to M.
Deshayes, essentially southern in their character and relations. This
formation is separated from the Chalk by the London Clay or its equi-
valents, and the Woolwich series and Thanet Sands, with the fauna of
which it has few species in common, whilst, as I have before men-
tioned, the species of the Lower Eocene beds have a more northern
facies. It is not, however, long since MM. Cornet and Briart found
under the equivalents of all these English series in Belgium a friable
calcareous bed full of fossils, not like those of the overlying Lower
Kocene, but resembling, and in many cases identical with, those of
the more recent Calcaire grossier. Again, in the Barton Clay, many
lxvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
species of the London Clay, which had disappeared during the period
of the intervening Bracklesham Sands, reappeared with the reoccur-
rence of argillaceous strata. One of the most remarkable cases, how-
ever, is that of the Argile de Boom, which forms the very top of the
Eocene series of Belgium,—the Oligocene of German geologists.
This deposit is so like the London Clay in lithological character
that it would be almost impossible to distinguish them, while the
shells (especially the several species of Yusus, Plewrotoma, and Natica)
so closely resemble those of the London Clay, from which it is sepa-
rated by the four or five divisions of the Upper Hocene, that they
might easily be mistaken for London-Clay fossils. The exeeptional °
appearances of Colonzes, whether in the older or newer roeks, are,
no doubt, mainly due to the recurrence at certain intervals of
similar lithological, thermal, and bathymetrical conditions.
During the Middle Tertiary or Miocene period, it would seem
that a different distribution of land and water prevailed. The
Miocene beds of Skye and of Greenland, with their remarkable
floras, indicate land and fresh-water conditions, while at the same
time the Miocene marine beds of France and Germany are rich in
subtropical forms of Mollusca. Assuming part of the area which
now constitutes the Northern Atlantic area to have been then dry
land, the migration southwards of arctic species of Mollusca would
have been for a time interrupted.
Approaching nearer to our own times, we have Pliocene beds in
Iceland, Quaternary deposits in Spitzbergen and on the western
flanks of the Scandinavian peninsula, while in this country Glacial
or Preglacial beds range to the height of from 1000 to 1400 feet
above the sea-level. There is reason, therefore, to believe that
the bed of the North Atlantic may have been from 1500 to 1600
feet or more deeper during the Pliocene and Glacial period than
it now is. If northern submarine currents are now checked, as
Prof. Wyville Thomson supposes, by the shallower seas between
Scotland and Greenland, such an addition to its depth as these
emerged portions indicate would materially have affected those con-
ditions, and have allowed of a freer passage of the north-polar
waters, and consequently of a freer dispersion of its fauna to the
abysses of the mid-Atlantic, where, in fact, so large a number of
them are now found to exist. This more open communication gaye
rise, I conceive, to that great; migration of northern Mollusca which
are now found fossil in Italy and Sicily, and some of which still sur-
vive in the Mediterranean and mid-Atlantic.
ANNIVERSARY ADDRESS OF THE PRESIDENT. lxix
It is more difficult to understand the absence of later Quaternary
shells, such as those of the Clyde beds, only three of which have
been recognized among the late dredgings. Does it arise from the
more littoral and shallow forms of that class being stayed by cli-
matal conditions near our shores, while the deeper-sea forms passed
on southward free from the influences which affected the others?
That a great proportion of the deep-sea forms had migrated during
and since that period is probable from their wide diffusion and large
numbers. Mr. Jeffreys has enumerated fifty of these more recent
northern Mollusca which are not known in a fossil state; and of
the Echinoderms and Crustacea mentioned by Dr. Carpenter and
Prof. Wyville Thomson a large proportion are Norwegian, Spitz-
bergen, and other high-northern forms.
From what I have previously said, you will have understood that,
lithologically, there is but little resemblance between the Atlantic
mud and our typical white chalk, none that could have ever led a
geologist into any error of determination. In fact, in no part of the
area yet explored is there any thing at all to be identified lithologi-
cally with the true white chalk. Even if it were found that the
superposition were conformable, the difference of mineral character
is too marked. At the same time it is to be observed that the area
of the Atlantic is so vast that, variable as the deposit now going on
seems to be, it is probably little, if any, more so than that which
went on in some parts of the Chalk series in the bed of the Chalk-
ocean over the old European area. Of the rate of the present de-
posit we know nothing. Is it even going on everywhere over the
deep Atlantic ?
Therefore, although I think it highly probable that some con-
siderable portion of the deep sea-bed of the mid-Atlantic has conti-
nued submerged since the period of our Chalk, and although the
more adaptable forms of life may have been transmitted in unbroken
succession through this channel, the immigrations of other and more
recent faunas may have so modified the old population, that the ori-
ginal chalk element is of no more importance than is the original
British element in our own English people. As well might it have
been said in the last century, that we were living in the period of
the early Britons because their descendants and language still lin-
gered in Cornwall, as that we are living in the Cretaceous period
because a few Cretaceous forms still linger in the deep Atlantic.
Period in geology must not be confounded with “system” or
“formation.” The one is only relative, the other definite. A
Ixx PROCEEDINGS OP THE GEOLOGICAL SOCIETY.
formation is deposited or takes place during a certain time; and
that time is the period of the formation; but a geological period
may include several formations, and is defined by the preponderance
of certain orders, families, or genera, according to the extent of the
period spoken of; and the passage of some of the forms into the
next geological series does not carry the period with them, any
more than would any particular historical epoch be delayed until
the survivors of the preceding one had died out. Period is an arbi-
trary time-division. The Chalk or the “ London Clay” formations
mark definite stratigraphical divisions. We may speak of the period
of the London Clay, or we may speak of the Tertiary period. It
merely refers to the “time when” either were in course of con-
struction. The occurrence of Triassic forms in the Jurassic series,
of Oolitic forms in the Cretaceous series, and of Cretaceous forms
in the Eocene, in no way lessens the independence of each series,
although it may sometimes render it difficult to say where one series
ceases and the other commences. The land and littoral faunas are
necessarily more liable to change than a deep-sea fauna, because an
island or part of a continent may be submerged and all on it de-
stroyed, while the fauna of the adjacent oceans would survive ; and
as we cannot suppose the elevation of entire ocean-beds at the same
time, the marine fauna of one period must be in part almost neces-
sarily transmitted to the next.
Thus while continental Europe and the sea-bed, as far as from 200
to 800 miles west of the British Islands, was subject to successive
changes of level, giving rise to a series of Eocene, Miocene, and
Pliocene strata with their diversified and varying faunas, the adja-
cent depths of the Atlantic may have continued with little variation,
except that produced by currents and relatively small differences of
depth. Of the nature of that deep-sea fauna we were until lately
entirely ignorant. At the same time it may be observed that
geologists held to the opinion of deep-sea deposits ; and the views
of EK. Forbes, with regard to the bathymetrical limits of life in the
sea, were by no means generally accepted. The Chalk, attaining as
it does a thickness of 1000 to 1500 feet, and having a special fauna,
was always looked upon by geologists as the deposit of a very deep
sea. Even supposing the conclusions of E. Forbes to have been
accepted, no geologist could have safely inferred, from a rock being
non-fossiliferous, that it had been deposited in a sea the depth of
which exceeded the limits he assigned to marine life. In the first
place, the sediment of which the rocks are formed may have been
ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxi
of a nature unsuited for the existence of life over the original sea-
bed. It is now evident that the absence of life in the depths of
the Aigean is due to the fine tenacious mud (which, by the by, E.
Forbes likened to chalk), in the same way that those areas of the
Mediterranean, discovered by Capt. Spratt, and of the Atlantic at
the entrance of the Straits of Gibraltar, discovered in the ‘ Porcu-
pine’ expedition, to be covered by fine mud, apparently in a state
of continual slow deposition, were found to be almost entirely barren.
On the other hand, where the rocks consist of sandy strata, any
fossils composed of carbonate of lime may have been dissolved
out, and all traces of them lost by the percolation of rain-water,
after their elevation into dry land, as happens in the Bagshot Sands,
in which it is only by chance in the few instances where the sand
happens to be consolidated by a ferruginous cement that the im-
pressions and casts of shells are preserved. Another well-known
cause for the absence of fossils in a sedimentary deposit is the
circumstance of the strata having undergone metamorphic action.
I should hardly have thought it necessary to mention these various
causes to account for non-fossiliferous rocks, but for a recently
expressed opinion of a presumed more general acceptance of Forbes’s
hypothesis amongst geologists than has been at all the case.
As bearing also upon the distribution of life in the same stratum
at points in near proximity, Dr. Carpenter notices that there are
areas in the North Atlantic in which the temperature varies con-
siderably at the same relative depths; and he infers that there are
permanent warm and cold areas, distinguishable not only by differ-
ences of from 10° to 15° of temperature, but also by a difference of
marine life, such as might present a geological difficulty. He notes
the presence of Globigerine and abundance of vitreous sponges on
a fine muddy bottom in the one, and of northern forms of Echi-
nodermata and Crustacea on a bed of sand and stones in the other.
Mr. Jeffreys, however, did not find the same difference in the Mollusca.
He states that the result of his examination shows that there are
forty-four species in the warm area and fifty-five species in the cold
area, and these latter included all the forty-four of the former; and
he accounts for the absence of Globigerina on the ground that “the
strength of the submarine current in the cold area is sufficient to
sweep away and remove these slight and delicate organisms,” which,
from later observations by other naturalists and himself, he believes
inhabit only the superficial stratum of the sea. The slight difference
in temperature seems hardly sufficient to account for the absence of
lxxil PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Gilobigerina in the cold area, while the extent of the other differences
loses much force by the identity of the Mollusca. We know not also
whether there is not a passage from one area to the other. We require
therefore more evidence before the geological value of the distinction
of the two areas can be fully accepted; at the same time the impor-
tance and interest of such an influencing cause must be kept in view.
I will now say a few words on one of the most important bear-
ings that these deep-sea researches have on chronological geology.
Objections have been taken on various grounds to the percentage
test of Sir Charles Lyell, as evidence of relative age. The data of —
the deep-sea dredgings furnish us with curious and apparently
paradoxical reSults and such as might seem fatal to this test. Sup-
pose an isolated portion of the deep-sea Atlantic bed had been ele-
vated at some late period, and that we were yet ignorant, as we were
only twelve years since, of what was to be found in the unexplored
depths of the ocean. Suppose further that the Atlantic deposit had
taken place on such rocks as the Paleozoic strata of Cornwall or
South Ireland. A chalky-looking deposit would then have been
found overlying old rocks, with nothing to indicate stratigraphi-
cally its geological position, and with fossils to a great extent new.
In the absence of a complete knowledge of the deep Atlantic fauna,
I will take, as a specimen of what they might have been, the result
of one deep dredging in 5964 feet. Mr. Jeffreys obtained in this -
single dredging 186 species of Mollusca. Of these he found :—
91 species recent or living.
24 ~,, formerly known as fossil only, and belonging to the Plio-
cene strata of Sicily ; some of these are undescribed.
71 ,, new or undescribed.
186
The conclusion would have been that 95 out of the 186, or 51 per
cent., were of extinct species ; and of these, 24 would be referred to
Pliocene age. What would have been the inference as to the age of
the beds? Certainly, on palzeontological evidence alone, there could
have been but one conclusion. They must have been classed as
Pliocene or older, although these researches have now shown all the
species to be recent.
The case, however, is an extreme and exceptional one. It is
true that, in future speculations, the possibility of such a case
happening must be taken into consideration ; but the depths of the
Atlantic are so great that, unless in case of a disturbance such as
that of the elevation of the Alps or the Andes, we are not likely
ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixxni
to find it brought before us in recent geological times*. Apart
from such an exceptional case, I consider that, if all disturbing
causes be properly taken into account, the percentage test is a
good and useful guide for the chronological arrangement of the newer
strata; nor, notwithstanding its exceptional character, do I con-
sider that a case like the one just referred to need perplex the
geologist, who would seek elsewhere, in superposition or In some
points of physical structure, for evidence as to place. Palseonto-
logy is an excellent counsellor, but it should always be kept sub-
ordinate to stratigraphical geology. It indicates what may be the
ease, but it does not tell us what must be the case. The one
has rigid, the other flexible lines; and these lines are rarely pa-
rallel. The geologist should first determine rigorously the order of
superposition, before he speculates on the distribution of the fauna.
Stedfast in that mode, there need be no cause for error, however
exceptional and varying the fauna may be. It is his business to
determine the fact, and then, with the aid of the paleontologist,
to discover the cause and amount of variation, and to detect the
principle on which the distribution of life in the period under
investigation has been regulated. Palzontology must be our guide,
but not our master. It is this which gives life and interest to so
many of the higher problems of paleontological geology.
In one point of view, the geologist has the advantage over the
naturalist. The latter examines the coasts and dredges in the
ocean, but he can only skim the surface, whereas the former has
the old sea-beds opened out to him. He can see, at any given
time, what has been below the surface. The dredge may pene-
trate a few inches; but the old shoals and shell-banks of the
Coralline Crag sea, for example, can be opened out to the depth of
10, 20, 30 feet or more, exposing the range of life both in time
and in horizontal distribution at any given epoch. What may be
under the surface of the Atlantic mud we know not. Is there a
suecession of strata extending down to the equivalents in time of
our chalk strata? or would the equivalent of the latter prove to
be merely one part. of a series, the other end of which would
convey us back to Oolitic, Jurassic, Triassic, or even to Carboni-
ferous times? Many of the forms of life indicate a sequence in
this great chain. Some of our present marine Foraminifera go back
* The absence of any known deposits in our Tertiary series of a character
like the present deep Atlantic mud is another proof that none of that part of the
old ocean-bed has been raised since the Chalk period.
VOL. XXVII. vii
Ixxiv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
to these Mesozoic and Palzozoic times ; and we know not yet what
further resemblances to old forms of life may yet be detected in
the vast field just opened to us.
The present explorations, full of interest and valuable as they
are, are insignificant compared with the vast area of the ocean ; so
that when we look at what has been accomplished in these tenta-
tive researches, we can only take them as indicative of the rich
mine that yet remains to be explored, and look forward to dis-
coveries that will probably modify and throw much new light on
the relations between the marine life of the present and the past.
One of. the great subjects which these researches may put before
us in this new light is, that instead of the imperfect record which
geology usnally gives us of the life of the old world, with its in-
terrupted succession in local descent, we may have, if the hypo-
thesis of an area continuously submerged from the Cretaceous
period should prove true, the lineal descendants of some portion of
those creatures which lived in the Chalk seas. If so, naturalists
will be able to see the exact amount of changes wrought, and to
study in what direction they have been effected. We shall see the
effects of continuity in time in conjunction with continuity of con-
ditions, and whether any and what new forms have been evolved,
and where no progress has been made. We see already that the
Foraminifera, Sponges, and Echinoderms claim relationship with
their fossil antetypes, though in an unequal degree. How will the
fully ascertained results agree with the theory of Natural Selec-
tion? Beautiful, ably handed, and ingenious as this theory is, it
seems to me—I will not say to fail, because I am not competent
to pronounce on the natural-history bearings; but it fails to sa-
tisfy me. Natural Selection is founded primarily on Sexual Se-
lection ; and this latter seems to me an implant so strong, and
to have an object so definite, viz. that of maintaining the species
in full vigour, strength, and health, that, in the absence of any
more direct evidence to the contrary, I would believe in the force
of this law of life to perpetuate the special type unaltered, rather
than in a divergent natural selection, leading, concurrently with
changes of condition, to aberrant forms. We have had curious
and remarkable evidence of elasticity of structure in certain direc- ~
tions; but does not the rebound, in almost all cases, show the
existence of a spring which, while it admits of considerable play,
tends to readjustment as soon as the restraint is removed. That
there have been gradual changes in structure in all classes of animal
ANNIVERSARY ADDRESS OF THE PRESIDENT.- Ixxyv
life, concurrent with the passage of time, is evident, especially to
geologists ; but of the way in which these changes have been carried
out, 1 own to not yet seeing a sufficient explanation. Have ter-
raqueous changes led to variations in the structure of animal life
by the law of Natural Selection among the few that best adapted
themselves to the changed conditions ? or was it by a gradual modifi-
cation induced in the many, in consequence of the general change
to which they were all subjected? or was there some law in time, or
of a character yet unknown to us, cooperating with the change in
conditions, to produce those singular and extraordinary changes and
variations of structure of which we have now such full evidence
as to fact, but so little as to theory ?
These are some of the problems towards the solution of which I
look with great hope in the continuance of these most interesting
deep-sea researches, important alike to the naturalist, the physicist,
and the geologist.
P.S. The few particulars in this Address relating to deep-sea tem-
peratures were collected some twenty years since for a paper never
published. As they form fitting antecedents to the more important
recent researches, I have incorporated part of them here, leaving
possibly some of the intermediate work rather incomplete.
Nore.—Since the greater part of this Address was printed, Mr.
Jeffreys informs me that he has now, through the kindness of Prof.
Lovén, examined the shells procured in the Swedish expedition of
1869 by dredging on the Josephine Bank and off the Azores, at
depths ranging from 110 to 790 fathoms; and that nearly all these
shells belong to the same species as those procured in the ‘ Porcupine ’
expeditions at similar depths.
t
tdek hat sthoelty viet’
THE
QUARTERLY JOURNAL
OF
THE GEOLOGICAL SOCIETY OF LONDON.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
Novemser 9, 1870.
Lieut. Reginald Clare Hart, R.E., Brompton Barracks, Chatham ;
Lieut. James Frederick Lewis, R.E., Brompton Barracks, Chatham ;
and M. F. Maury, Jun., Esq., 1300 Main Street, Richmond, Vir-
ginia, U.S., were elected Fellows of the Society.
The following communications were read :—
1. On the CarzontrErous Frora of Bear Istanp ce 74° 30’ N.).
By Professor Oswatp Husrr, F.M.G.S
[ Abstract. |
Tue author described the sequence of the strata supposed to belong
to the Carboniferous and Devonian series in Bear Island, and indi-
cated that the plant-bearing beds occurred immediately below those
which, from their fossil contents, were to be referred to the Moun-
tain Limestone. He enumerated eighteen species of plants, and
stated that these indicated a close approximation of the flora to
those of Tallowbridge and Kiltorkan in Ireland, the greywacke of
the Vosges and the southern Black Forest, and the Verneuwilii-shales
of Aix and St. John’s, New Brunswick. These concordant floras he
considered to mark a peculiar set of beds, which he proposed to
denominate the “‘ Ursa-stage.” The author remarked that the flora
of Bear Island has nothing to do with any Devonian flora, and that
consequently it and the other floras, which he regards as contempo-
raneous, must be referred to the Lower Carboniferous. Hence he
argued that the line of separation between the Carboniferous and
* The publication of this paper is deferred.
VOL. XXVII.—PART I. B
2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
Devonian formations must be drawn below the yellow sandstones.
The presence of fishes of Old-Red-Sandstone type in the overlying
slates he regarded as furnishing no argument to invalidate this con-
clusion. The sandstones of Parry Island and Melville Island are
also regarded by the author as belonging to the “ Ursa-stage,”
which, by these additions, presents us with a flora of seventy-seven
species of plants. The author remarked upon the singularity of
plants of the same species having lived in regions so widely separated
as to give them a range of 263° of latitude, and indicated the rela-
tions of such a luxuriant and abundant vegetation in high northern
latitudes to necessary changes in climate and in the distribution of
land and water.
Discussion.
Sir Cnarztes Lyprt remarked that the Yellow Sandstones of Dura
Den in Fife, and of the county of Cork in Ireland, contain Glyp-
tolepis and Asterolepis, genera of fish exclusively Devonian, or be-
longing to the middle parts of the Old Red Sandstone—also the
genus Coccosteus, which is abundantly represented in the Middle
Old Red Sandstone, and sparingly, or only by one species, in the
Carboniferous formation. The evidence derived from these fishes
inclined him to the belief that the Yellow Sandstone, whether in
lreland or Fife, should be referred to the Upper Devonian, and not
to the Lower Carboniferous, as Sir Richard Griffiths contended, and
as Heer now thinks.
As to the argument founded on the plants, he considered it an
important and truly wonderful announcement, that many well-
known Carboniferous species are common to Bear Island (in lat. 74°
30' N.), in the Arctic regions, and to Ireland and other parts of
Europe (26° of latitude further south). But fossil plants are supposed
to have a wider range in space and time than fossil fish ; and we know
that the cryptogamic flora of the ancient coal is remarkable for the
wide horizontal spread of the same species, extending from North
America to Europe, so that we need not be surprised if many
species should extend vertically from the Devonian into the Carbo-
niferous strata.
Mr. CarrurHers remarked on the bearing of the paper on the
Kiltorkan beds, and considered that Dr. Heer had completely esta-
blished the correlation of the deposits. He differed, however, as to
the numerical proportions of the species. He could not recognize
Cyclostigma as a genus, but considered it founded on insufficient
erounds, in which view Prof. Haughton now agreed. It was, in
fact, founded on fragments of the bark of Lepidodendron Griffithsii,
Brongniart, to which species the Lepidodendron indicated by Prof.
Heer as L. Velthetmianum really belonged. Other detached por-
tions of this same plant had been described by various authors
under no less than seven different specific names, and referred to
nearly an equal number of distinct genera; and Prof. Heer had
reckoned these as species in his comparison of the Bear-Island and
1870. ] WOOD—WEALD-VALLEY DENUDATION. 3
Trish floras. Prof. Heer had been led, chiefly by the erroneous de-
termination of the Kiltorkan Lepidodendron by the Irish palzonto-
logists, to refer these beds to the Carboniferous rather than to the
Devonian formation, the Kiltorkan fossil haying been established as
a very distinct species by Brongniart and Schimper. Mr. Carruthers
considered that both the Irish and Bear-Island deposits belonged te
the Devonian.
Mr. Boyp Dawxrnys pointed out that the proximity of land was
exhibited by the presence of terrestrial plants in the deposits, and
prevented the correlation of the inshore deposits with those which
were being formed in deep water. As the marine fauna changed
more rapidly than the terrestrial flora, it was preferable for classi-
ficatory purposes. He mentioned forms of vegetable life assigned
by Dr. Heer to the miocene which had really been discovered
in America in beds of Cretaceons age. He did not believe that
corals could have existed in those high latitudes under any thing
approaching to the present conditions. Prof. Nordenskjold had failed
to discover any traces of glacial action in these beds ; and the ques-
tion arose whether there had been any change in the position of the
Pole or whether the heat radiated by the earth was sufficient to
render an Arctic climate equable in Paleozoic times.
2. On the KyipEence afforded by the Durritan Brps without and
within the NoRTH-EASTERN PART of the VALLEY of the WEALD as to
the Movs and Date of the Denupation of that Vattny. By 8. V.
Woon, Jun., F.G.8.
[Prats I.]
Tue denudation of the Weald valley has long been a subject of
interest and of contention among geologists. The theory of a rise of
a dome of strata from beneath the sea and the offthrow of the waters
on all sides from that dome, their escape through lateral fractures
in the upheaved chalk, together with a slow wearing back of the
fractured and denuded edges of the chalk in the form of cliffs, long
held its ground in our text-books, and it is only of late years that
this theory has met with partial dissent.
Sir Roderick Murchison was the first*, I believe, to bring pro-
minently into notice the fact that a large part of the débris con-
tained within the denuded area consisted of angular chalk flints
brought from the exterior into the inner part of this area, and so
far therefore was at variance with the received hypothesis of a flow
of the denuding waters outwards from the exposed subcretaceous
strata, over the surface of which these flints were scattered. His
view, after an elaborate description of the detrital beds of, more
especially, the western part of the great valley, was that the denu-
dation had been accomplished by a powerful aqueous agent directed
eastwards from the apex or western extremity of the Weald valley,
by which these flints have been thus scattered over the Neocomian
strata of that part of the valley.
* Quart. Journ. Geol. Soc. vol. vii. p. 349. 3
B
4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
Another elaborate memoir treating of the detrital beds within the
Wealden escarpment, and their bearing upon the mode in which the
denudation was effected, is that of Messrs. Foster and Topley*.
The view of these gentlemen was that after a plane of marine denu-
dation had been effected over the original area, the whole of the
denudation by which, not merely the valleys proper of the Wealden
rivers, but also the great excavation of the Weald itself (or major
valley), with its well-known contour, have been accomplished was
effected by these rivers, especially the Medway, flowing in their
present direction—a view indorsed, apparently, by Prof. Ramsay rf.
Many other notices, special and incidental, upon this question
have appeared, and among them notices from Mr. Martin, Mr.
Godwin-Austen, Mr. Prestwich, and Mr. Mackie; the first-named
of whom has for a long period been a staunch upbolder of the
marine theory; while Sir Charles Lyell, itis well known, has always
adhered, in his ‘ Elements’ and in his ‘ Manual of Geology,’ to the
same hypothesis of marine agency.
In 1866 a study of the distribution of the gravel of the Thames,
of that of East Essex and its continuation in the lower valley of the
Medway, and of that of the heights above Canterbury led me
to the conclusion that each of these gravel-sheets had partaken of
some of the movements by which the Lower Tertiaries upon which
they rest had acquired their present position and outcrop, and had
thus been contemporaneous with some portion at least of that earlier
part of the Wealden denudation to which the removal of the Ter-
tiaries from the North Downs is due.
I then called especial attention to the circumstance that the posi-
tion of the Thames and East Kssex gravels in their troughs precluded
the possibility of a connexion between them and the Thames river,
either in its present or any prior condition, because that part of the
Thames valley which lies east of Gravesend, instead of being coinci-
dent with the gravel-troughs, cuts at right angles through them—a
feature also possessed by the next river to the north, the Crouch,
the valley of that river, as well as the portion of the Thames
valley just referred to, being entirely destitute of gravel or brick-
earth.
These features, I pointed out, necessitated an admission that the
troughs in question had their seaward terminations in the direction
of the Weald, because the trough which contained the Thames
gravel was absolutely shut in from the north sea by the lofty ridge
which separated it from the East-Essex sheet, that ridge not having
been opened for the river Thames to reach the North Sea until such
* Quart. Journ. Geol. Soe. vol. xxi. p. 443.
+ Physical Geology and Geography of Great Britain: 1863 & 64.
{ See papers on the Structure of the Thames Valley and its contained Depo-
#5 in vol. iii. of Geol. Mag. pp. 57 & 99, and paper on the Structure of the
Valleys of the Blackwater and Crouch, and of the East-Hssex Gravel, and on the
yelation of this Gravel to the Denudation of the Weald, zd. pp. 348 & 398 ;
also on the Postglacial Structure of the South-east of England, in Quart. Journ.
Geol. Soc. vol. xxiii. p. 394.
1870.] WOOD—WEALD-VALLEY DENUDATION. 5
a late period as that when the conditions giving rise in these parts to
gravels and brick-earths had ceased—the period in fact of the modern
alluvium, which alone oceurs in the valley, or more properly the
wide gorge thus cut through the ridge.
I then pointed out that east of London, where it occupied the
more seaward portion of the channel thus opening southwards towards.
the Weald, the Thames gravel had been greatly broken up, denuded
and elevated irregularly, by which action partial terraces had been
formed—that under these terraces occurred the gravels and brick-
earths of fluviatile origin with Cyrena fluminalis which had succeeded
to the spreading out of the gravel occupying such terraces—and that
these were the deposits of rivers into which the original gravel-inlets
had by the elevation of their bottoms become reduced, such rivers,
equally with the inlets that had preceded them, opening to a sea in
the direction of the Weald. The mouths of these rivers, I considered,
had followed the shore-line as this gradually receded southward from
the rise of the Wealden area, until the sea, first becoming confined
within an estuary of its own eroding, marked by the Wealden
escarpments, was eventually expelled from the Wealden area—and
that upon this event taking place, the drainage acquired its present
reversed direction from the Weald into the Thames estuary, which
then came into existence*.
At the time when by a study of the gravels without the Weald I was
thus led to these views, I had not examined with any detail how far
the constitution and position of the gravels lying within the chalk
escarpments supported or conflicted with them. This I have now
done, so far as concerns the north-eastern part of the area, which,
from its contiguity to the mouths of the Thames and East Hssex
gravel inlets, is the part of principal importance in the question ; and
I propose now to show its bearing upon it.
In doing so it will, I think, be advantageous to consider also a
question that I had deferred for the occasion, viz. how far the
theories of the denudation of the Weald by agencies which involve
the escape of the material removed in the course of denudation out-
wards from the Weald and into the Thames area, be they atmo-
spheric, fluviatile, or marine, receive support or meet with negation
from the composition of the detrital beds lying without the north-
eastern part of the Weald.
Taking up this latter inquiry first, we have two sets of detrital
beds to consider, viz. the Glacial and the Postglacial. Of the first,
we have in this part of England two formations, the Boulder-clay
and the gravel underlying it, which I have termed Middle Glacial.
In neither of these deposits can it be said that the débris of the
* In my paper in the Quart. Journ. Geol. Soc. vol. xxiii., at p. 408, I regarded
the brick-earth of Erith and Crayford as distinct from that of Grays, and as
having preceded the Thames gravel. Finding afterwards, by a clearer section,
that it did not pass under that gravel, I, in a letter published at page 534 of the
fifth volume of the Geol. Mag., withdrew from that position, and admitted that
the Grays and Erith and Crayford Brick-earths are identical, and belong alike
to the lower terraces of the Thames-gravel formation.
6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9
Wealden denudation is represented. In the gravel (which is com-
posed of chalk-flint, with a considerable percentage of quartzites)
there occur fragments of other rocks, among which are some of
chert, sandstone, and limestone, that may possibly belong to rocks
within the Weald, though I am not aware that such an origin can
be with any certainty affixed to them. Again, Mr. Prestwich men-
tions having found fragments of chert and ragstone that he refers to
the Lower Greensand of Kent in the shingle of the cliff near South-
wold, belonging to the Glacial formation.
Such occurrences as these, however, afford no ground for conclu-
ding more than that prior to the Glacial epoch such a planing off of
the Wealden area had begun as to afford exposures of the beds
beneath the chalk, from which some fragments might at the com-
mencement of the glacial period have found their way into gravels
then in course of formation. The evidence necessary, however, to
justify any assumption that the Weald valley existed as a subaerial
tract during the whole Glacial period must go very far beyond this.
Whether we suppose this valley to have been occupied during the
Glacial period with ice which streamed through the lateral valleys
of the north-east side into the Thames area—or whether we suppose
it to have had a milder climate, so that rivers of water instead of ice
followed the same course—in either case great volumes of the wreck
of the subcretaceous strata ought to have been brought into the
glacial beds which approach so near to the Wealden area as do those
of the south of Essex; but these beds, especially the Boulder-clay,
are conspicuous by their absence. If we consider through what various
beds of stone the Medway and Darent valleys are cut, and what
immense quantities of this stone must have been removed to form
them, the absence or extreme paucity of such débris in the Glacial
beds is significant; but if we couple, as we have been asked to do,
the denudation of the great valley of the Weald itself with the ero-
sive action of the Wealden rivers, then this becomes still more signi-
ficant, and the impossibility of the Weald haying been under sub-
aerial conditions during the prevalence of those excessively detrital
agencies that we attribute to ice seems to me obvious—and the more
especially when we remember the greater extent which the Lower
Greensand formation must have occupied in the earlier stages of the
Wealden denudation, all of which, with its great beds of stone in
fragments, has gone somewhere.
Further, the Boulder-clay of the Essex heights is mainly com-
posed of rolled chalk ; but it is not the soft chalk of Kent and Surrey,
but the hard chalk of Yorkshire and Lincolnshire, termed “ Rock”
by the well-borers of those counties. The flank of the Lincolnshire
chalk-wold for a long distance is occupied by a vast deposit of
glacially degraded chalk, so pure as to be extensively quarried for
lime, and so thick that the range of country formed out of it rivals
in height the Wold itself. We thus see to what sort of detrital
accumulation a range of chalk hills has given rise under the powerful
action of glacier ice; and it appears to me but reasonable to expect
something of the kind to have occurred over the south-east of Eng-
1870.] WOOD—WEALD-VALLEY DENUDATION, 7
land, had that region been under subaerial conditions during the
prevalence of this icy envelope; yet, after allowing for the excessive
denudation which has, as it seems to me, prevailed in postglacial
times over the south-east of England, the complete absence of the
smallest vestige of any such accumulation as we find in Lincolnshire
is, I think, reconcilable only with the conclusion that during the
formation of the Boulder-clay this region was covered by the sea—
a conclusion, moreover, to which the position of the Boulder-clay at
elevations of 300 feet and upwards on the Essex heights that front
the North Downs equally points.
So far, therefore, as the evidence of the detrital beds of Glacial
age lying without the north-eastern part of the Weald affords a test,
we are, I think, entitled to infer that the Weald was not during the
climax of the Glacial period an area undergoing denudation by streams
either of water or of ice, and, indeed, that, with the exception of the
earlier part of that period, it was not above water at all. .
Passing now to the Postglacial beds, the principal formations of
this age lying without the Weald are the gravels to which I have
already made allusion under the names of the gravels of the Thames,
of East Essex, and of the Canterbury heights.
Precisely the same kind of reasoning is applicable to these as to
the case of the Glacial beds, so far as concerns the débris of sub-
eretaceous rocks. If the Stour, the Medway, and the Darent,
running outwards from the Weald, had effected any thing like the
prodigious denudation attributed to them, fragments of the stone-
beds of the Lower Greensand ought to make up at least half the
volume of the Thames, the East-Essex, and the Canterbury-heights
gravels where these three streams pass through them.
In the Thames gravel of this part, however, such fragments,
though common, form but a small proportion of the gravel mass, the
bulk of which is flint with some quartzites intermixed. The Kast-
Essex gravel, both where it lies within the valley of the Medway
between the Nore and Rochester, and where it extends along the
east coast of Essex, presents similar features; while the gravel of
the Canterbury heights, which forms the sides of the valley through
which the Stour flows, is even more exclusively flint in its compo-
sition, as it requires a search of some time to find half a dozen frag-
ments of any other material, so that in this gravel the proportion
of any other material than flint is probably not +,)55 of the mass.
If we reflect how small is the elevation of these gravels above the
streams which flow beneath them, in comparison with the elevations
which the suberetaceous rocks attain within the Weald, can it be con-
tended that gravels so composed could have been deposited from rivers
which were effecting the enormous denudation that has placed these
rocks as they now are? Can we, even if we reject the hypothesis of
this great fluviatile denudation, reconcile the composition of these
gravels with their deposition from these rivers when in greater volumo
than now?
The answer seems to me to be clearly negative, and that under such
‘circumstances the flint in the East-Kssex gravel between Rochester
8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
and the Nore ought to form but a subordinate proportion of the
constituent material, while in the Canterbury-heights gravel nearly
as much subcretaceous material as flint ought to occur. The case
of the East-Essex gravel, especially of that part of it which extends
from the Nore to Rochester, is a very strong one ; for the chalk forms
but avery small part of the area drained by the Medway, and, while
the gravel-producing material, the flint, constitutes only a small per-
centage of any given amount of chalk strata removed, especially of
the Lower Chalk which obtains in this area, the portion of the Lower
Greensand formation which is drained by the Medway is largely
made up of beds of hard stone. The Hastings-Sand formation, too,
abounds with indestructible gravel-forming material, and in as large
a ratio at least as does the chalk. Omitting the Weald Clay and the
Gault as non-gravel-forming strata, we have, roughly speaking, the
following proportions borne by the areas of those gravel-producing
formations lying beyond the LHast-Essex gravel termination at
Rochester whose drainage falls into the Medway, viz. :—
Lower London Tertiaries ............ 0-25
(Unt ia dete MA As tah ie meek wes Aa Alene falta 1:00
ihower Grecnsanae en els te eee 2-75
astmeaspoawds ee een ene ine meee 3°00
opal ne ety ter 7:00
While the chalk thus figures for only one-seventh in area, it would,
in proportion to any given quantity of strata-removed, yield no more,
indeed less, of flint than the Lower-Greensand beds, or even the Hast-
ings-Sand formation, would of hard gravel-forming material.
If it be objected that the stone beds of the Lower Greensand are
mostly limestone, and therefore soluble under the action of acidulated
water, such objection does not apply to the Hastings-Sand material,
of which, indeed, the broad sheet spreading over the Weald-Clay bot-
tom is mainly, and in some parts exclusively, composed. Neither
has it prevented the gravels of the Lower Greensand country from
being principally made up of the stone beds of this formation.
Moreover, the Kentish Lower-Greensand Limestone, so extensively
used in building, is not of a perishable nature, and much of it is in
that broken condition most suitable for supplying fragments for
gravel-accumulation; while on the other hand so perishable a
material as the Kentish Chalk has, according to Messrs. Topley and
Foster, found its way, in the form of nodules, into gravels near
Maidstone. Allowing, therefore, the fullest weight to this objection,
can we resist the admission that if the Hast-Essex gravel, especially
that part of it lying between Rochester and the Nore, resulted from
the transport of the Medway, the flint débris in it (exclusive of the
Lower Tertiary pebbles) should be largely outbalanced by subcreta-
ceous material, instead, as the case is, of that material forming but
a very small proportion of this gravel? This inference will not be
appreciably weakened by supposing that the respective escarpments
extended southwards in former time, because a careful examination of
1870.] WOOD—WEALD- VALLEY DENUDATION. 9
a map of the drainage-areas and of the elevations will show that the
proportions borne by the Chalk, Lower-Greensand, and Hastings-
Sand superficies would then remain pretty nearly the same as now—
the chief sufferer by such extension being the Weald Clay, owing to
the steep upthrow possessed by the Hastings-Sand formation.
The question then naturally arises, how did any fragments having
their parentage within the Weald get into these gravels unless there
was an outflow from the Weald? The explanation offering itself is that
the tidal flow up the inlets in which I regard these gravels as having
been deposited would bring such material in moderate quantities from -
any exposures of the parent rock within the Weald; and I may ob-
serve here how little effect geologists seem disposed to attribute,
whether in the way of transport or of denudation, to this powerful
and uniform force—the tide. It seems to me that the character and
contents of the main mass of the gravels of the Thames, East Essex,
and Canterbury heights, composed as they are almost wholly of flint
in all stages of wear, from the subangular fragment down to the
spherical Lower Tertiary pebble*, is far more consistent with a de-
rivation from the wear of a long coast-line of Lower Tertiaries and
Chalk than with a derivation from rivers draining, as those of the
Weald do, extensive areas of subcretaceous strata abounding in stony
beds.
I now propose to consider the case of the detrital beds within the
portion of the Weald here under consideration.
As before mentioned, Sir Roderick Murchison has shown the great
extent and quantity of angular chalk flmt which is scattered over
the Lower Greensand of the western extremity of the Weald, and that
flint and Lower-Greensand débris, with some Tertiary pebble, zs
scattered over the Weald-clay zone drained by the Eden. In the
north-eastern part of the Weald, although angular flints are abundant,
the gravels which I regard as anterior to those resulting from the
present rivers are more or less mixed with pebbles derived from the
Lower Tertiaries.
The especially noteworthy feature connected with this intermix-
ture, however, is that the pebbles and the angular flint present no
intermediate grades of rolling to connect them ; so that it is obvious
this admixture of angular flint and tertiary pebble cannot, in finding
its way to the positions it occupies, have undergone any considerable
or repeated amount of wear by transportt. ‘This feature seems to
me repugnant to any presumption that these pebbles have settled
* Tn this respect the Lower or Fluviatile gravels of the Thames sheet differ
greatly from those of the main mass, as their flints are far coarser and more
angular, and present less gradation towards the Tertiary pebbles mixed with
them.
+ Instances occur, moreover, in which chalk fragments have occurred in this
intermixture. Considering how impossible it is for chalk to sustain without
dissolution any long-continued aqueous action, this circumstance is also of much
importance. The difficulty is enhanced in the case of one of the gravel patches
shown in the map as resting on Weald clay west of Yalding, in which Messrs.
Foster and Topley speak of chalk nodules having occurred. Their transport
there, however, by drainage, in the reversed condition shown in the map, seems
to me simple enough.
10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
down into their present places by successive transport from higher to
lower levels during a long-continued fluviatile denudation—because
such a successive and long-continued transport could not have failed
to grind the smaller pebbles into sand, and to reduce the angular flints
into all stages of wear, connecting them with the pebbles themselves.
In the map accompanying this paper, some of the more elevated
gravels within the escarpments of the part of the Weald under con-
sideration which are characterized by the presence of an admixture of
chalk flints and Tertiary pebble, are shown in a way which dis-
tinguishes them from the rest of the gravels there. Of these, such
as fall within the area drained by the Medway or its afiluents,
have been described by Messrs. Foster and Topley*. The rest,
lying within the drainage-area of the Stour, I will briefly notice.
About Kennington, near Ashford, these occupy a high position,
far above the Stour, and distant about a mile from it. The bulk of
the Kennington gravel is composed of suberetaceous material; but
there is a considerable proportion of angular flint in it, and some
Tertiary pebble.
On the opposite side of the Stour, at Willesboro’, is a remarkable
patch exposed in the road-cutting west of the village. So far as I could
detect, upon a brief examination, this gravel, 5 feet thick, was almost
entirely made up of Lower-Tertiary pebbles and fragments of flint.
At Smeeth, three miles further west, and midway between Merstham
Hatch and Ridgeway, there is a gravel of subcretaceous material,
intermingled with flint and Tertiary pebbles and a few pieces of
chalk ; and over the gault belt near to the chalk escarpment, angular
white-coated flints often occur lying on the surface, but apparently
no Tertiary pebbles.
The position of these gravels near Ashford, and of those above
Maidstone, relatively to the chalk escarpments near each place, and
to the rivers Stour and Medway, is indicated by the Sections A and
B that accompany the map; and the Sections have their places indi-
cated by lines upon the map. In both cases these gravels he near
what I regard as river-mouths bringing in drainage from the north ;
while similar gravels, described by Messrs. Foster and Topley, lie
within the Medway area on the Weald clay beneath the Lower
Greensand escarpment, and occupy a position near what I fegard as
one of these river-mouths after it had advanced from the Chalk es-
carpment at Maidstone to the Lower-Greensand one near Yalding.
In the case of some of the gravels near Maidstone, Messrs. Topley
and Foster offer, as the explanation of the occurrence of flints, nodules
of chalk, and pebbles in them, the action of a rivulet tributary to
the Medway, which runs up towards the foot of the Chalk escarp-
ment at Boxley. But though angular flints and chalk might by
such a means find their way into the Medway, it is not apparent how
Lower-Tertiary pebbles could do so, even at the greatly higher level
at which both the tributary and the Medway itself must have flowed
to reach the high situation of these gravels at Barming, and above
Allington (near Maidstone).
The position of the gravel at Willesboro’ is still more antagonistic—
* Loe. cit.
1870, | WOOD—WEALD-VALLEY DENUDATION. 11
because, though composed of angular flint and Tertiary pebbles, the
stream that passes Willesboro’, a tributary of the Stour, does not
reach any way near to the chalk escarpment, while pits in the Lower-
Cretaceous stone are close at hand. In striking contrast with this
Willesboro’ gravel is the gravel skirting the Stour at lowest level at
Bucksford, less than three miles west from that at Willesboro’.
This low-lying gravel is entirely made up of subcretaceous material,
though by long search a solitary fragment of flint may be found in
it, derived probably from the flints scattered over the Gault surface,
up to which some of the rivulets running into the Stour extend ; it
is obviously a deposit of the Stour when flowing in greater volume
in the same direction as at present. But, looking at the physical
and geological features of this part of the Weald, can it be con-
tended that a similar flow at from 50 to 100 feet higher level could
have deposited gravel of such opposite character to this as is that
hard by at Willesboro’ or that, about 15 miles distant, on the heights
at Canterbury ?
I would, however, prefer to deal with the possibility of these
pebbles reaching such positions on broader grounds than the precise
position of the rivulets nearest to their place of occurrence ; that is, I
regard their position as repugnant to any introduction from the Stour
or Medway, in their present direction, during the course of a pre-
longed atmospheric or fluviatile denudation which resulted in the pro-
sent excavation forming the Weald, for the following reasons, viz. :—
1st. The form and character of the great Wealden denudation
area (or major valley), as distinguished from the valleys proper of the
Wealden rivers (or minor valleys), is diametrically opposite to any
that can result from river-action, because, however great we concede
the power of that action to be, any excavation resulting from it must
be conterminous with the excavating agent itself (the river and its
tributaries), since every stream, large or small, can only deepen its
own proper valley, and the result cannot be any such excavation as
the major valley of the Weald, with its well-known contour and
escarpments, but only a series of valleys, or minor excavations,
ramifying in the directions in which the stream extends, and in some
degree at least comciding with them; and the longer this action is
continued, the deeper and more distinct must these features become.
2nd. If flints and pebbles were derived from the Chalk escarp-
ment, we should look for an increase in their number as the escarp-
ment is approached; but though a few angular flints are in some
places scattered over the surface of the Gault, the Lower-Tertiary
pebbles seem wholly. absent from that part of the area, and from the
sources of the streams supposed by some to have brought them.
3rd. The Lower-Tertiary beds yielding pebbles are far away from
the escarpments, and rest on the northern extremity of the chalk
slope and below the crests of the escarpments; and however high
the level be to which we carry our imagination of the flow of the
Wealden rivers in past times, even if up to the level of the escarp-
ment-top itself, still the drainage from the Lower-Tertiary strata
must at all times have flowed away from the scarp, and not into the
Weald. There are, however, some patches of pebble-beds (of date
12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9, .
prior to the excavation of the Weald valley, whether of Lower
Tertiary age or of some subsequent period) which occur near to,
and even on, the chalk escarpment, and are shown in the accom-
panying map. ‘These, however, clearly could not have supplied the
pebbles to the Kennington, Willesboro’, and Smeeth gravels, which
lie within a separate drainage-area—that of the Stour; and if we
suppose those gravels that are shown in the map as lying within the
area of the Medway drainage and containing Tertiary pebbles to have
been supplied from this source (straining our imagination, and ig-
noring, in order to do so, various physical features that conflict with
such a direction of supply), we ought for consistency to find Tertiary
pebbles in increasing proportions in those gravels of the Medway
drainage-area, both higher and lower, which lie nearer and nearer
to these scarp beds; but such is not the case.
While the introduction of these pebbles, and the nature and form
of the area of denudation seem to me alike repugnant to any con-
ceivable river-agency acting in the direction of the present streams,
the position and mode of occurrence of all the gravels within this
part of the Weald appear to me to be just what might be expected
from the sequence of events after the Thames gravel which I have
in previous papers put forward; and this sequence I will endeavour
here to trace in harmony with the composition and position of such
gravels.
I should premise, in order to remove misapprehension, that I have
never entertained, and wholly reject, the hypothesis of the escarp-
ments having ever been cliffs, although they appear to me to have
formed sea-margins and steep foreshores*. The absence, however,
of beds with contemporaneous marine fossils within the Weald, either
at the feet of the escarpments or on elevations within the major
valley, does not seem to me to be entitled to any weight; for there
is proof, from the envelopment of some two or three miles of it in
Boulder-clay, that the escarpment of the Yorkshire Wold existed
during the glacial period, and must therefore have been a sea-mar-
gin, because, in whatever way this Boulder-clay was formed, no one
can deny that the Yorkshire Wold passed under the Glacial sea; and
if the valley below it was filled with, and the Wold covered by, ice
when subsiding, they were clear of this when emerging, and under-
went great denudation during that process. The features exhibited
by sections of mine, Nos. 7 & 8, at p. 402 of the 23rd volume of the
Society’s Journal, render it difficult to deny that the same thing oc-
curred with respect to the chalk-escarpment of Herts and the lower
grounds below it. Nevertheless we do not in either of these cases
meet with beds with marine fossils referable to this period of emer-
* While rejecting the hypothesis of scarps being in any way allied to cliffs, I
cannot admit that the absence of beaches at their feet is any argument in the
case, because hundreds of steep acclivities in the north of England and in Scot-
land that could not have been any thing else than cliffs when emerging from the
glacial sea, are quite destitute of beaches at their feet. Some of these, such as
Gristhorpe cliff in Yorkshire, shown by me and Mr. Rome in section at p. 180
of the 24th volume of the Quarterly Journal, have now become cliffs again, and
have the beach at their feet, which they had not when rising out of the glacial
Bea.
1370.] WO0OD—WEALD-VALLEY DENUDATION. ~ 13
gence and denudation. The Glacial beds of Hast Anglia have un-
dergone a similar emergence and denudation; and even those who
attribute the Wealden denudation to atmospheric and fluviatile
agencies admit that the Lower Tertiaries and Chalk over the south
of England underwent a previous denudation or planing off by marine
agency; but where are the beds with marine fossils in Kast Anglia
or over the south of England representing such emergence and de-
nudation? ‘These questions might be extended to the denudation
of the coal-measures and other old rocks; but the phenomena pre-
sented by denuded area$ appear to me to show, uniformly, that a
denudation effected during upheaval* is unrepresented by beds with
contemporaneous marine fossils deposited over the denuded area.
Upon any introduction afterwards of the sea, however, we get
these beds—as, for instance, the Kelsea gravel in Yorkshire, the fen-
gravels of East Anglia, and the brick-earth of the Nar in Norfolk :
but there has been no such reintroduction of the sea into the Weald
since its denudation, unless it be in the Lewes levels. The beds
with marine fossils contemporaneous with the Wealden denudation
are to be looked for without the Weald, 2. ¢. beyond the region of
upheaval and denudation ; and thus it is, as well as for the other
reasons assigned in the sequel, that I refer the fossiliferous mud-bed
of Selsea, lying in the depressed and wndenuded fold between the
two areas of upheaval and denudation, the Isle of Wight and the
Weald, to the period of that upheaval and denudation.
In the accompanying map, by means of shading in the escarpment
carefully reduced from the ordnance map, the very conspicuous
features of mouths opening towards the Weald, presented by the
gorges in the chalk escarpment between Guildford and Dover, and
by that in the Lower-Greensand escarpment at Yalding, are made
apparent t. The gorges of the South Downs present no such feature.
Now patches of gravel containing Tertiary pebbles occur near
one or other of these mouths: and it is clear that streams flowing
from the north through the Tertiary and Chalk area, and debouch-
ing through these mouths into a sea occupying the area within
these escarpments, would necessarily bring an abundance, both of
angular chalk-flint and of Lower-Tertiary pebbles into the Weald,
there to intermingle with fragments having their parentage within
the Weald itself.
My proposition is that the violent disturbances from east to
west at some time subsequent to the older Tertiaries to which, it is
universally admitted, the Weald owes its present form? took place
* Tt is the reverse with denudation during depression; for there the advan-
cing sea, as ¢. g. that of the Lower Tertiaries over the Chalk, planes off its floor
‘and then deposits its sediment with contemporaneous marine organisms—pre-
ceding this usually, however, with beds of rolled fragments.
+ To show better the physical features of the scarp, the strip of Atherfield
clay that forms the foot of the Lower-Greensand escarpment has been shaded in .
with the Weald clay, instead of, as is usual for geological grouping, with the
Lower Greensand.
+ In order not to encumber the case discussed in the body of the paper, I have
14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 9,
subsequently to the accumulation of the Thames gravel, and that
their effect was to put an end to that gravel and the coeval gravels
of East Essex and of the Canterbury heights, and gradually to raise
the sea-bed over Kent and Sussex, and away to the north of France,
giving rise thereby to a great submarine denudation—that by this
action the inlets in which the Thames and coeval gravels had accu-
avoided reference to any earlier stages of the Wealden denudation. Mr. Prest-
wich, in his ‘Memoirs on the Lower London Tertiaries,’ gave reasons for sup-
posing that the first elevatory action over the Wealden dome preceded the Lower
Tertiaries. Those also who agree with him as to the age of the Lenham and
Paddlesworth beds, must admit that a considerable planing off of the chalk,
exposing probably the subcretaceous strata, was renewed prior to those Lenham
and Paddlesworth beds being deposited. I would again call attention to the
physical fact, plain to any who will take the trouble to extract the contours from
the ordnance map, that there are two distinct sets of disturbances traceable in
the south-east of England :—one, the sharp rectilinear east and west upthrows,
by which the denudation of the Weald valley has been induced, and which I
consider to have affected the Thames gravel, both east and west of London, and
to be connected with the similar upthrows of the Isles of Wight and Purbeck (all,
therefore, of a date posterior to the first accumulation of the Thames gravel) ;
and the other, a set of anterior origin, consisting of a series of concentric curves,
the exterior of which is formed by the Cotteswold escarpment, and the next to
that by the chalk escarpment from Pangbourne to Royston, while the inner ones
constitute a series of smaller escarpments, of which the trumpet-mouthed gorges
in the North Downs, referred to in the paper as river-mouths, successively form
parts, the whole set centring near Canterbury. These curves are connected
very distinctly with another, and apparently contemporaneous, set, which centre
near the western extremity of the Isle of Wight, and are concentric half circles
formed by the Lower-Tertiary outcrop of Hampshire and the chalk escarpments
of the south-west. The rectilinear movements to which the denudation of the
Weald valley is due, have destroyed this anterior curvilinear contour, which is
perfect up to the points where these rectilinear upcasts occur. I formerly sup-
posed that these curved groups were, equally with the rectilinear ones, of post-
glacial origin ; but an examination of the glacial beds of Bedfordshire and of
Northamptonshire showed these beds in such a position relatively to the chalk
and oolite escarpments (which form successive concentric curves of the Can-
terbury group) as necessitated the inference that the curves were of preglacial
origin. ‘These curvilinear movements appear, however, to be clearly synchro-
nous with the first denudation of the Tertiaries from the south of England, and
with that planing off of the chalk over the Weald, to which allusion has been
made. The two principal rectilinear flexures, by which the direction of the
denudation of the Weald valley has been induced, are those of Portsdown Hill
and the Guildford Hog’s-back ridge, running east and west and parallel to each
other, and indicated by lines in Map No. II. The upthrow of these I consider
to have so acted on the sea expelled from the north of Kent by the synchronous
upcast of the country from there over to France, as to have caused it to denude
their regular parallelogrammatic trough formed by the chalk escarpments of
the Weald. The two inner curves of the concentric series which centres at
Canterbury are visible on the accompanying map, No. I., the innermost of
the two being formed by the escarpment which skirts the Canterbury-heights
gravel on the west, and extends down to the Weald escarpment above Smeeth.
The northern extremity of this curve has now disappeared into the north sea.
The other, and next outward curve, is formed by the escarpment which skirts
the East-Essex gravel on the west, and extends down to the Weald trumpet-
mouth above Maidstone. The two trumpet-mouths west of this are successively
partial repetitions of these curves; but the next. complete repetition is made
by the chalk escarpment from Pangbourne to Royston; and the next to this,
and last, is the Cotteswold escarpment, prolonged by the oolitic escarpment
through Warwickshire, and by the oolitic escarpment of Northamptonshire.
1870. ] WOOD—WEALD-VALLEY DENUDATION. 15
mulated shrank into river-channels, through which the drainage of
Essex and Middlesex flowed southwards to this disturbed sea. In
order to make this intelligible I have placed beside the larger map,
which shows the detrital beds and contour surface, two smaller ones
illustrating the succession of events thus supposed. ‘The first of
these shows the distribution of land and water when the Thames and
coeval gravels were accumulating, and the other this distribution
when the sea had deserted the chalk country and retired within the
chalk escarpments of the Weald.
Now, in addition to the three openings in the North Downs,
through which the rivers Stour, Medway, and Darent flow, and
which expand trumpet-mouthed towards the Weald, and are regarded
by me as the remains, first of old channels, and afterwards of old
river-mouths, there is another precisely similar mouth further to the
west, through which the Brighton Railway passes. This mouth
forms now a dry valley extending from Croydon to Merstham, but
so elevated and shallow in comparison with the three others that
the railway has to pass out of it into the Weald at Merstham by
means of a tunnel. Elevated and destitute of water as is this
trumpet mouth, it is identical in form with those through which the
rivers Darent and Medway flow, showing undeniably, as it seems to
me, that this trumpet-shaped feature is not due to the erosive action
of a river flowing outwards from the Weald, for no river at all is
there.
The explanation of this dry, shallow, and elevated trumpct
mouth seems to me to be this, viz. that itrepresents another of
the channel-, and eventually river-mouths opening into the Weald
which became established when the sea was retreating to the chalk
escarpments. :
As we go eastwards from this point, the chalk and Lower Green-
sand have an easy dip; but as we go westwards from it the dip
becomes much sharper, until between Guildford and Farnham the
chalk is all on edge, and at angles varying from 35° to 45°. It seems
to me therefore that while this more easy upcast eastwards permit-
ted the fluviatile wearing down combined with tidal erosion to keep
pace with the upcast, and so maintain these mouths as points of
river discharge, the more abrupt character of the western upcast did
not allow of this being done; so that the drainage into the Weald
through this trumpet mouth, traversed by the Brighton Railway,
was put an end to at an early stage in the retreat of the sea Weald-
wards. The gorges through which the Mole and Wey now flow were
probably similar mouths, which (although the sharpness of the
chalk upcast in their neighbourhood has somewhat destroyed their
trumpet-mouthed character, as well as the coast-contour that was
synchronous with them) nevertheless were cut through during the
disturbances so as to allow the drainage to flow into the Weald.
That part of this easterly drainage which flowed through the
Darent gorge seems to have terminated before the Lower-Greensand
escarpment became the sea-margin; but that flowing along the lines
of the Medway and Stour remained unarrested, the mouth of the
16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
Medway drainage having been worn down step by step as the Lower-
Greensand escarpment rose above the waters, until it presented the
condition now exhibited by the trumpet-mouthed gorge cutting
through that escarpment at Yalding; at which time, or even pre-
viously, through the opening in the Lower-Greensand hill to the
north of them, the Lower-Tertiary pebbles and angular flints abund-
antly present in the gravels near that place, shown in the map,
were thus brought from the northward through the Lower-Green-
sand escarpment.
The Lower-Greensand escarpment subsides and disappears near
Ashford; so that where the Kennington, Willesboro’, and Smeeth
gravels containing the flint and pebble admixture occur, there is no
such escarpment at all. The mouth by which the drainage through
the Stour valley entered the Weald seems therefore not to have much
advanced beyond the chalk escarpment; so that the gravels at these
places represent both the gravels above Maidstone, accumulated
when the Medway mouth was near the chalk escarpment, and the
gravels about Yalding, accumulated either about the same time or
else later, when that mouth had become established near the Lower-
Greensand escarpment. The highest of the Stour area, viz. those
at Kennington, seem to be probably coeval with the gravels above
Maidstone; while those of Willesboro’, which are at a lower level,
may be synchronous with the gravels about Yalding.
During the later portion of this change the Hastings-sand country
formed, it seems to me, a large island, so that what for convenience’
sake I have called sea, was really only an inlet receiving freshwater
through these several rivers ; and since the width between this island
and the chalk escarpment varies only from eight to eleven miles, and
between it and the greensand escarpment from five to six miles only
at the narrower parts, there would have been a considerable tidal
scour exerted under any circumstances, while the far greater volume
of the land-drainage of those postglacial times, compared with what
now obtains in the east of England, would tend to push the limit of
fresh water further out into estuaries than at present. Great
freshets too, carrying with them volumes of river-mud with its
associated organisms, would be poured into the Weald; and through-
out it is to be remembered that the fresh water must follow the
salt water as the latter recedes by the extension of the shore-line,
and occupy its place. In this way it seems to me that there would
be nothing repugnant’ to the events I have traced, if the gravels in
question should hereafter be found to yield the remains of land or
fresh-water organisms, such as do occur in some of the gravels and
brick-earths shown in the map under a different shading, and which
are most of them due to the rivers flowing as they do now.
The views thus sketched assume the Weald, when the sea had retired
within the chalk escarpments, to have been the island-studded head of
a still longer inlet formed by the British Channel while this channel
was closed to the north by an isthmus between Dover and Calais,
which had come into existence by means of that elevation of the
chalk country which put an end to the Thames gravel and its coeval
1870. | WOOD—WEALD-VALLEY DENUDATION. If
beds. This assumption I brought forward in 1866*, when first
endeavouring to show the process by which I consider the Wealden
denudation to have been accomplished,: n ignorance that it had
been already, as I find, suggested by Mr. Mackie+. The sug-
gestion, however, when fitted into its proper place as to time, 2. e.
posterior to the Thames gravel, appears to me an essential ingredient
in the proposition, because the existence of such a barrier between
the Channel and the North Sea must have largely augmented the
tidal rush and consequent erosive action of the waters within the
Weald. On the other hand, the diminution of this tidal scour,
produced by the opening of the Dover Straits, supplies an efficient
cause why the elevation of the Wealden area should overmaster the
denuding agency, and so extricate the Weald altogether from the
sea.
It may be further added that this state of things agrees with the
features of the marine deposit skirting the sea between Selsey and
Worthing, in Sussex, described by Mr. Dixon and by Mr. Godwin-
Austen. A numerous fauna has now been obtained from this deposit
by Mr. A. Bell, which, while it is quite unlike that of any of the
glacial deposits, and also unlike any of the marine postglacial depo-
sits in other parts of England, and in Scotland +, nevertheless con-
sists entirely of species that are still living. Nearly all the shells
are denizens of our extreme southern shores; but a few do not reach
us, having their northern limit on the Lusitanian coast, so that this
deposit indicates that at some Postglacial period the British Channel
was subjected to an influx of Lusitanian water, which afterwards
ceased and was followed by a change, under the influence of which
certain Lusitanian mollusca disappeared from our shores. This
order of succession is shown by the deposit in question being over-
lain$ by a few feet of deposit containing some large angular erratics.
This overlying erratic deposit, I take the opportunity of ob-
serving, I regard as quite unconnected with the glacial beds,—its
erratics being due to the presence of conditions of climate such as
introduced the large angular blocks into beds of the Thames gravel
series at Grays, the greywether blocks into the Postglacial gravel
of Hampshire, and the boulders into the Postglacial clay of Hessle,
in Yorkshire,—such deposits being due to conditions of climate
wholly unlike those which gave rise to the Greenlandic conditions of
the Glacial period, but similar to what now obtains in the Gulf of
St. Lawrence and other parts where ice forms on coasts during the
winter. The deposit, however, may perhaps indicate a colder sea-
* Geol. Mag. vol. iii. p. 402.
t Geologist, vol. iii. p. 203.
{ I group all the Scotch so-called Glacial shell-beds as Postglacial, as they
rest on the Boulder-clay, and have a very different fauna from the Glacial beds
proper, which include the Boulder-clay on which these Scotch beds rest.
§ Godwin-Austen, Quart. Journ. Geol. Soc. vol. xiii. p. 49. According to
Mr. Austen the fossiliferous deposit has large portions of the skeletons of
Elephas primigenius imbedded with the shells, and is underlain by red gravel.
This gravel may probably, therefore, belong to the age of the Thames beds, or
nearly so.
VOL. XXVII.—PART J, c
18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
water than that underlying it, in which the Selsey fauna lived;
and this colder change I associate with the admission of the North
Sea through the Dover Strait.
So soon as by these means the elevatory action gained on the
tidal erosion, and the Weald was deserted by the sea, the reversal of
the drainage of the Stour and Medway into its present direction
commenced. Its first result would be that the streams, descend-
ing from the northern portion of the Hastings-sand country, and
having to seek a new outlet, would form a lacustrine kind of ex-
panse up to the level where a point of outlet along the present line
of drainage was found for it. The deposit of that expanse I trace
in the wide-spread sheet of gravel which skirts the Medway and its
tributaries, the Beult, Eden, and Teise, over the Weald-clay bottom,
and which, in the case of the Beult and Teise, is formed almost ex-
clusively of material derived from the Hastings-sand country, locally
called ‘“‘Crowstone gravel,” but which in the case of the Eden, as
Sir Roderick Murchison has shown*, has a considerable admixture
of Lower-Greensand and flint material, and, in the case of the Teise
(as I am informed by Mr. Topley), of Tertiary pebbles also, derived, I
conceive, from the prior distribution of such material over the area
when in the condition shown in sketch map No. ILI.
A few patches of gravel resting on Weald-clay, but occupying
higher ground than this sheet, skirt the Hastings-sand country, such
as those at Marden and Wantsuch Green, mentioned by Messrs.
Foster and Topley. These are similarly composed of Hastings-sand
material; and though these gentlemen speak of flint having been
found in them, it must be excessively rare; for I could not detect
a trace of it. Their age I regard.as similar to that of the gravels
with Tertiary pebbles about Yalding and at Willesboro’; but being on
the opposite side of the channel formerly occupying the Weald-clay
area, they received no Tertiary pebbles like their coeval gravels at
Yalding and Willesboro’, but were supplied by the material de-
scending from the Hastings-sand hills. The few flint fragments
that Messrs. Foster and Topley speak of may have drifted along the
island shore from those abundant accumulations of flints described
by Sir Roderick Murchison, which are scattered about the more
western parts of the Weald. These patches are considerably above
the great sheet skirting the Beult, and are divided from it by a
slope of bare Weald-clay.
The gravels and brickearths which fringe the valley of the Med-
way between Maidstone and Chatham, and of the Stour between
Ashford and Canterbury, occupying lower levels than the gravels
with Tertiary pebbles, already specially discussed, are more difficult
to distinguish, as it is obvious that any earlier gravels or brickearths
deposited at low levels in these valleys before the drainage was
reversed, would, after that event occurred, become undistinguishably
mixed up with the deposits from such reversed drainage.
The same remark equally applies to those lowest accumulations of
gravel and brickearths which fall within the Thames, the Hast-
* Quart. Journ. Geol. Soc. vol. vii. p. 381.
1870. ] WOOD—WEALD-VALLEY DENUDATION. 19
Essex *, and the Canterbury-heights drainage-areas, because a similar
intermingling must have resulted in these cases. Nevertheless, look-
ing to the fact that there is an absolute absence of gravel or brickearth
in the valleys of the Crouch (notwithstanding its tributary rivulets
extend up to the heights capped with glacial beds, which would have
supplied some gravel material) and of the estuary of the Thames,
which, as already described, have been excavated at a late period
through the high ridge separating the Thames from the Kast-Essex
gravel-sheet, and through those sheets themselves—and looking to
the feebleness of the gravel conditions exhibited by the wide sheet
skirting the Medway and Beult, to which allusion has been already
made, it is probable that by the period of this reversal the condi-
tions giving rise to the formation of brickearth and to the transport
of gravel by such flat-falling streams as the Thames and Medway
had ceased in a great degree, and given place to those different con-
ditions to which the river-mud or modern alluvium is due; so that,
save to the extent of rearrangement by the action of the river-
waters, when more voluminous and at higher levels than now, most
of the material of the gravels along the lower levels of the Medway
and Stour valleys, except the sheets skirting these rivers and their
tributaries within the Weald, was probably transported before the
reversal took place. In the case of the Darent, inasmuch as its rever-
sal seems to have preceded the retreat of the sea within the Lower
Greensand escarpment, its gravels would be much more due to the
rivers while flowing in their present direction than would those of the
Stour and Medway, because at this earlier stage the conditions giving
rise to gravel and brickearth had not so nearly passed away:
It may be asked where, if it be not represented in the gravels lying
without the Weald, has the débris of the subcretaceous rocks re-
moved to form the valley of the Weald gone? The most probable
answer seems to me to be that it is distributed over the bottom of
the English Channel—not in the modern superficial shingle, but in
the form of thick beds far out to the west covered by the modern
shingle, and concealed by it and by the waters of the Channel.
To sum up the case as I have endeavoured to put it, we have the
following propositions :—
Ist. The absence from the Glacial beds of Essex of any débris
representing a considerable denudation of the Weald during the
Glacial period, and grounds, in the position and constitution of the
Boulder-clay of the Essex heights, for regarding the Wealden area
as beneath the sea during the accumulation of that clay.
2nd. An absence from the principal Postglacial gravel sheets
outside the north of the Weald of any quantity of Lower-Cretaceous
or Hastings-sand material, adequate to represent the Postglacial de-
-nudation of that valley by any agent that involves a transport of
the material removed into the area occupied by these gravels.
* That is to say, the portion only which occupies the Medway valley between
Chatham and the Nore; the portion on the north side of the Thames, viz. in
Hast Essex, would, unless the North Sea at this time still remained at some
distance from the Thames mouth, be exempt from this later intermixture.
c2
20 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Nov. 9,
3rd. The difficulty of reconciling the presence of Tertiary pebbles
in certain Wealden gravels with an origin by means of rivers flowing
in the direction of the present ones, however high we imagine those
rivers to have been.
4th. The antagonism between the character and form of the
major valley of the Weald and that of any conceivable excavation
which could result from the agency of rivers, not merely from rivers
coincident with the present ones in direction, but from any rivers
at all.
5th. The proof which the position of the gravels of the Thames,
of Kast Essex, and of the Canterbury heights, and especially the po-
sition of the lofty ridge dividing the Thames and EKast-Essex gravels
from each other, furnishes that the sea of this gravel-period was to
the south of these gravel-sheets.
6th. The circumstance that the old coast-contour, when the sea
lay within the Weald, and the channels and river-drainage entered
it from the north, remains now stamped, as from a die, on the Chalk
and Lower-Greensand escarpments, except in the particular region
where that on the chalk was obliterated by the excessive marine
denudation consequent upon the acute upthrow of the Guildford
Hogsback—especially the dry inlet mouth at Merstham.
7th. The natural manner in which the gravels with Tertiary
pebbles, mentioned in proposition no. 3, fall into their places, if they
be regarded as having received these pebbles by means of channels and
rivers from the north; and the sufficient explanation whieh a tidal
indraught from the south, when the shore-line was chalk, and the
principal denudation of the subcretaceous strata not yet accomplished,
offers for the small quantity of subcretaceous material and enormous
quantity of flint possessed by the Thames, East-Essex, and Canter-
bury-heights gravels.
8th. The existence of a cause, in the shape of an isthmus at
Dover, which was adequate to induce a tidal scour sufficient, with the
river-flow from the north, to produce a denudation of the form and
character which the major valley and the minor valleys together
present ; the equally adequate cause for a cessation of this denuda-
tion, and for the mastery so attained by the elevatory action over
the denudation, which the opening of the Dover Straits (generally
admitted to be of a late Postglacial date) furnishes; also the general
fitting in of all these propositions with one another, and with the
features presented, on the one hand, by the very recent opening of
the mouths of the Thames and Crouch through the great ridge, and
the absence from the valleys of the Thames mouth and of the Crouch
river of either gravel or brickearth ; and, on the other hand, by the
character of the Selsey deposits.
Note explanatory of the Map (PI. I.).
In order that the physical features may appear, the Atherfield-
clay has been shaded in with the Weald-clay, instead of, as usually,
with the Lower Greensand.
The lines A and B indicate those of the two sections, A and B, which
; NO IT. Quart. Journ. Geol. Soc Vol. XXVILELL
rv of Land and Water atier the termination of the Thames
sea had retired withan the Wealder Chalk Escarpment.
ATUO
SO
y YL
Z hy Bills 7F 7, CZ re Ls
Pal : Zae yf Y
SS
WY
7,
lL lthalk. WZOlderTertiaries. & @ Pebble beds
Gravels older thar the Thames & allied sheets.
aves Gravel formation where distinguishabie tronv the mainmass,
“gant and Tertiary pebbles, referred to the period wherthe Droinage
f these contarr tlt and Tertuary pebbles) E22 )Gravels, &c.
NB. Allayum and Modern Shingle omitted.
et The lines numbered 4, 5,10, 11, 13, 14 and 15 indicate those
aaiteees ITAL. aggre i, "IW EsCorpmerts, Ttudges and Valley slopes.
OAV AWAR SVW. Ir del
LAE
- ae
N° If. O Quart. Journ. Geol. Soc. Vol XXVILFLL.
Of the Distribntion, of Wa the Distributt ee if
Ak CEU a an Me The Ei Gravel, Period, whe the retired, whine Peaeae Caen es
NO! Te
Map of ‘The Detrital beds, Surtice contour,
i and Drainage syst ns within end without
{dhe North casterwpa -t of the WEALD,
Ulustratii xg paper by
S.ViWood |, Inrh: Gs.
SECTION 4.
Malle scarpmar Heath Woods The Medway. psc setae
= Ta TEED SM a =
: fs ae SECTION B. P é
ee ee
REFERENCE TO SECTIONS A&B. 1. Gravels, rete
ed) by Drarnag L
Z i Teterred to the Pertod when the Dramage was trom the Nord into the Weald.
\ re-arranged eu us present direction, The Challe and Suberetaceous Str, z Io
Pe 2. Gravels and Brickearths due to or
ata as iv Map NO
REFERENCE TO MAP N°]. :
Hastings Sand. = Weald. and Mherield, Gays. SQower Greensand, Gault and. Upr Greensand. (Challe. E7OlderTertiaries. © 8 Phble beds
quer necs the Cally escarpt . EX The Uppr Glacial ay. TES) The Middle Glach sand & Gravel, BBA Gravely older thaw the Thames & allied. sheets.
FEGravels &o, of the Thames, East Essex, and of the Canterbury heights E=ANawer. becls of the Thames Gravel. formation where distinguishable trom: the main mass,
ecther by the existence ofa terrace, or by thepresence of Oeste EBB ealden Gravels with, Mint and Tertiary pebbles referred’ to the period, nage
vas fromthe Noridu into the Weald. AWealden, Grawels of the later part. of the same period. (Some of these Contam flint and: Tertiary pebbles) E2@IGravels, &.
both: mithin and-without the Weald, which are daw (0, or re-arranged. by drainage tn tts present. direction, NB. Allavium, and Modern Shingle omitted.
, The tines with, barbed ends, are those of disterbance which have passed, trough: the thames gravel, The lines rambered: 4, 5,10, 4, 13, 19 and 15 indicate those
; % : ra of Sections with corresponding ruumbers at pages 398,406, 409, 42 and M5 Of the 23°°Vol. of the Journal. None = ~~ E'scarpments, Ridges and. Valley slopes.
eS : Ba SUM Trdele
=| 7 \ ! ve
ets 2 i 7
HA
1870.] WOOD—WEALD-VALLEY DENUDATION. 21
accompany the Map; but those numbered 4, 5, 10, 11, 13, and 14
indicate the lines of the sections given by me at pp. 394 to 417 of
the 23rd volume of the Quarterly Journal of the Society, which
have corresponding numbers attached to them there.
The two small maps are intended to make intelligible the changes
of the distribution of land and water to which I trace the denuda-
tion of the Weald. The first (No. II.) is intended to represent an
earlier stage, viz. that when the higher gravels of the Thames, Hast
Essex, and Canterbury heights were being accumulated in inlets
filled with salt water, and before the conversion of those inlets into a
fluviatile condition had heen effected by means of elevation. In
this the higher elevations of the North and South Downs and
of the Lower-Greensand country are represented as islands, the
wear of whose shores and of the Lower-Tertiary and Chalk inlet
shores supplied with some Lower-Greensand material the large
accumulations of flint and pebble that make up the Thames and East
Essex gravels, and supplied the flint to the Canterbury gravel. The
highest ridges of the Hastings-sand country are also represented as
islands. In the river-beds into which the more northern parts
of these inlet channels became converted, accumulated the Brick-
earths with Cyrena fluminalis, occurring at Clapton, Ilford, Erith,
and Grays within the Thames inlet, at Clacton and (according to
the President’s statement in the discussion) east of Southend in the
Kast-Essex inlet, and at Chislet in the Canterbury area, This
shell, unknown from the south or south-west of England, regarded
by me as mostly under the sea during this period, ranges north to
Yorkshire over the country regarded by me as land. During the
transition period preceding the establishment of these Cyrena-rivers,
those angular blocks (said to be Greywethers) occurring at Grays in
a brickearth on the slope above the Cyrena-deposit, but a little below
the great sheet of Thames gravel covering the plateau, would seem,
to have been carried in on ice by tidal action*.
The elevation, and the consequent shrinking and partial breaking up
of these inlets so as to form river-channels, I regard as a first result of
the disturbances under which the sea so retreated as to cause the
distribution of land and water to become eventually as represented
in Map No. III.f The upthrow of the Guildford Hogsback ridge
and of the ridge of Portsdown Hill (shown by lines on Map No. II.),
* These blocks are clearly not derived at second-hand from the Glacial beds
of Hssex, as supposed by Prof. Morris (Geol. Mag. vol. iv. p. 63); for they are
numerous, all alike, generally with sharp fractures, and all collected in one small
area; whereas in the Glacial beds of Hast Anglia large blocks are not common,
and what there are consist of divers rocks, and are mostly rounded.
t The commencement of the disturbances of which these rectilinear and
highly inclined ridges are the intensified result was, I consider, coincident with
the rise of England from the glacial sea, and the cause of the great denudation
effected during that rise over both the south-west and the south-east of England.
The margin of this complete denudation is distinctly marked by the abrupt ter-
mination of the glacial beds, at altitudes exceeding 300 feet, on the Essex heights
overlooking the Thames valley. Over the region south of these heights it is
obvious that, besides the glacial beds, a considerable mass of the older tertiaries,
and probably also much of the chalk and subcretaceous strata, were removed
—————
e
22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
contemporaneous, as I consider, with the similar rectilinear ridges
of the Isles of Wight and of Purbeck, represent, I submit, the
elevatory influences under which the chalk area of Hampshire and
of Wilts became converted into land, and under which the Wealden
upeast acquired that special configuration which gave to the up-
channel tide its great scouring power. In No. III. the sea is shown
as confined within the chalk escarpments of the Weald, with a barrier
of land extending across to France and shutting off the British Channel -
from the North Sea; while a part of the area now occupied by this
sea between Kast Anglia and the north of France was in the condition
of land supplying streams that found their way through the Stour
and Medway gorges into the Weald, so much of the drainage as passed.
through the Thames valley * reaching the Weald through the gorges of
the Wey and Mole to the west. The gravel-beds, with remains of an
ancient beach, described by Mr. Prestwich and by others near Calais,
appear to me to fall into their place between the two stages thus re-
presented, while the Brighton bed seems to belong to the period re-
presented by No. III. and to that following it. It will not be difficult
to pursue the change from the stage thus represented in No. III. to
that when the shore had become established at the Lower-Green-
by this preliminary postglacial denudation; while to the north of the Essex
heights, away to the northernmost extremity of Britain, the parts once covered
by the same glacial sea, being remote from the theatre of these disturbances,
felt their influence only in the form of a tranquil elevation, and were consequently
only partially denuded of their covering of glacial beds. It was during a lull
in these disturbances, and when this preliminary denudation and emergence had
brought about the conditions represented in Map no. IT., that the Thames gravel
accumulated ; so that more properly it was a renewal, and not the setting-in
of these disturbances, which, first completing the sharp inclination of the recti-
linear ridges, then lifted them, together with those portions of the chalk and
subcretaceous districts which had not yet emerged, above the sea, and, by re-
newing the causes of denudation, removed this accumulation everywhere except
in the places where we now find it (which it seems to me were the parts of least
disturbance at the particular epoch), eating also still deeper into the old strata as
they underwent elevation from the waters. I have elsewhere (Quart. Journ. Geol.
Soe. vol. xxiv. p. 174) endeavoured to connect this renewal of disturbance in the
south with the setting-in of that depression in the north of England to which
was due the postglacial clay of Hessle, which wraps like a cloth the deeply de-
. nuded glacial beds, and is underlain by a gravel containing the characteristic
shell of the Thames beds and their allies, the Cyrena fluminalis.
* The amount of drainage collected in the Thames valley east of London at
this period could have been but small, because the ‘entire bottom of this valley,
east of London as far as Erith, which is now occupied by the marsh mud, and
which, if the embankment were removed would be all flooded, is covered by
an oak, yew, hazel, and fir forest, rooted into the gravel and overspread by the
marsh mud. It is clear from this, that subsequent even to the latest part of
that gravel, but prior to the general depression of England, which buried so
many forests remaining round our coasts, as well as the forest in question,
the bottom of this valley, far within limits that, but for the embankments,
would now be water, was dry ground, It is this depression of so much of
England, at a late period, that I associate with the opening of the mouths of
the Thames and Crouch, and the occupation by the present North Sea of the
large area to the north of Kent, shown in Map No. III. as land. This general
depression seems to have been the recoil from the termination of the Wealden
elevation. ‘
1870. ] WOOD—-WEALD-VALLEY DENUDATION. 23
sand escarpment, with the Medway and Stour stil] discharging into
the Weald. All that remains, then, is to imagine the land to the north
of Kent depressed coincidently with the continued elevation of the
Weald, so as to produce an opening through the Straits of Dover*
and the introduction of the North Sea, where it now is, with the
denudation of the Thames and Crouch mouths taking place synchro-
nously with the desertion of the Weald by the sea, and the condi-
tion of things under which the drainage would acquire its present
direction is then attained. The terrestrial surface described by
Mr. Godwin-Austen as underlying at one place gravel of the Wey
seems intermediate between the desertion of the Weald by the sea
and the introduction over the spot of the waters of the river Wey,
which came into existence by means of that reversal.
In all this, I can but see the most ordinary and gradual changes
that must take place wherever land under the influence of active
subterranean disturbance is changing its level, pushing back the sea
in one place and admitting it in others; and that the elevation of
the Weald was accompanied by energy so active as to force the
whole thickness of the chalk into the Guildford Hogsback ridge is a
matter of universal admission. As this has admittedly occurred
since the Kocene period, is it at all incredible that it should have
taken place since the Glacial period? considering that beds whose
fossils indicate a parallelism with the Crag and earlier Glacial beds,
have become elevated in Sicily into mountain tracts. The Oxus
has deserted its bed within historical times, and now follows another
course to the Caspian.
Postscr1Pr.
Since the foregoing paper was sent in, the Journal of the Society,
no. 104, containing Mr. Codrington’s well-considered paper on the
Hampshire and Isle-of-Wight deposits, has appeared (vol. xxvi.
p- 528). The carefully prepared sections given by that gentleman,
illustrating the position of the gravels which cover so much of the
Hampshire Tertiaries, have an important bearing upon the subject
of the present paper, and seem to me powerfully to corroborate the
mode of origin and conditions of sequence which, in the present and
former papers, I have endeavoured to substantiate in the case of the
gravels of the London area.
It will be seen that the whole of the great gravel sheet illustrated
by Mr. Codrington’s sections is, like the Thames, East-Essex, and
Canterbury-heights gravels, cut off abruptly by denudation on lofty
brows towards the chalk country ; while in the opposite direction it
descends gradually from these brows towards the sea.
While the gravels of the London area, having been formed in
inlets, are necessarily thus cut off on brows towards the chalk
* T think it probable that the land between Kent and Calais was low in the
central part, the Wealden elevation having been least in the easterly direction.
The wearing back of the cliffs to the point where they cut across the chalk escarp-
ment is a subsequent process still going on.
24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 9,
country in those directions only where the inlets opened to the sea
(the gravel within the inlets remaining comparatively undisturbed),
the Hampshire high-brow gravels are everywhere so cut off in the di-
rection of the chalk country—as they would be, supposing them, as
I do, to be a remnant of the open sea-bottom of the period. All the
numerous sections given by Mr. Codrington present this feature ;
and though they omit the delineation of the older Tertiaries upon
which the gravels rest, an examination of the distribution of these
tertiaries as delineated in the Hampshire maps of the Geological
Survey will show, by comparison with the sections of Mr. Codrington,
that the gravels here have partaken, along with the tertiaries upon
which they rest, of that denudation which was consequent upon the
upeast of the chalk country. Mr. Codrington regards these gravels
as the deposit of an estuary of the sea, some twenty miles wide, that
was bounded by the chalk country to the north as land; and so I
agree they were, but not at that early stage when the gravel cap-
ping the brows of elevation (to altitudes of 400 feet and upwards)
rose out of the sea. At that time the gravel of the Hampshire high
brows stretched, I conceive, across the chalk country into connexion
with those gravels of the Thames, East-Essex, and Canterbury sheets
which now occupy similar brows of denudation, the conditions of land
and water being those represented in Map No. II., save that there
may have been many islands of chalk over Hampshire that I have
not ventured to represent. The marine denudation, consequent
upon the upcast of the chalk country, swept off this continuous
gravel sea-bottom from the parts subjected to the principal elevatory
movements, and cut back the older tertiary outcrops, with their
gravel covering, into the condition of brows just discussed, such
brows being lifted above the sea. To the south, towards the South-
ampton water, the but little disturbed sea-bottom continued to receive
and preserve gravel accumulations, which formed a more or less con-
tinuous sheet with the gravel which had become land on the brow-
tops ; while to the north, in the Thames valley, the waters, now con-
verted into the fluviatile condition, continued to deposit gravel and
brickearth, which inosculated with those portions of the earlier or
marine deposits that had remained undisturbed, but formed terraces
beneath the earlier-deposited gravel where this had been elevated *.
I here reproduce a reduction of section 10 of my paper in the
23rd volume of the Society’s Journaly, placing beside it one taken
from Mr. Codrington’s section 6, but extended so as to reach the chalk
country, and having the older Tertiaries inserted in it—in order that
the identical features which the gravel brows of either area present
* These marked terraces, where they exist in the Thames area, are shown in
Map No. I., and the lower terrace deposit indicated by a different set of dots
and lines from the main-sheet gravel. Where no such marked terrace exists,
the older and newer portions of the Thames gravel are shown necessarily under -
the same kind of dotting.
t In the original section the denuded shelf separating, along the line of section,
the gravel on the brow from that at lower level (with which, however, it inoscu-
lates in other directions) was not shown ; but itis corrected in the present section.
1870.]
Fig. 1.—The Aspect presented by the Gravel Brows of the Thames and Hampshire Areas towards the Chalk Country.
Section No. 10 of 8. V. Wood, Jun., from vol. xxiii. p. 406.
‘SOLIVIQAAT, VTTys
-due yy oy} Wor UopuoT
ey} suyeredes Aaqun09
HVYO ysry Jo [earoquy
Section No. 6 of Mr. Codrington extended to the Chalk country.
—_——_——$— a
Southampton
Thames at
WOOD—WEALD-VALLEY DENUDATION. 25
Petersham.
Combe House.
Chilworth.
Water.
i
-
N
‘
RG
x
WN
iy
i
Fe
:
BS
:
tt
5. The Bracklesham Beds.
3, London Olay. 4. Lower Bagshot.
a, a. The respective Gravels of the Thames and of the Hampshire sheets.
1. The Chalk. 2. The Thanet and Woolwich beds.
in relation to the chalk country
that separates them may be more
readily apparent.
Further, Mr. Codrington shows
that these gravels cap, in the form
of outliers at an altitude of 400
feet, the chalk ridge stretching
from east to west through the Isle
of Wight, the elevation of which,
like that of the Hog’s Back and of
Portsdown Hill, followed, as I
contend, the Thames gravel, and
was coeval in its formation with
the upeast of the chalk over the
south of England. The double sec-
tion (page 26) will make more in-
telligible the views which I hold
of the relation of the two gravel-
areas to each other, its direction
being indicated by a line on Maps
II. and III.
The upper representation shows
the condition of the Chalk and
Tertiaries after the Glacial period,
and the removal.by denudation of
the glacial beds, whose brow of
denudation occupies the northern
side of the Thames at elevations
reaching to upwards of 300 feet.
The removal of the Tertiaries
and Chalk had been partially ef-
fected by this same denudation,
but mainly effected by that pre-
glacial denudation associated with
the curvilinear configuration to
which, in the footnote at pages 21
and 22, allusion has been made.
This upper representation is
that of the state of land and water
in Map IT., while the lower shows
the same after the upthrow in
which the rectilinear ridges of
Portsdown Hill, the Guildford
Hog’s Back, and of the isles of
Purbeck and Wight originated.
By this upward movement the
chalk country was converted into
land, the sea confined within the
Weald: on the one side, and Mr.
Codrington’s inlet established on
the other; while the part of the
ana
26 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 9,
tertiaries nearest the surface became elevated with their gravel cover-
ing, and cut back by the denudation into the form of scarped brows.
While, however, the high brows of the Hampshire grayel are
thus, I contend, coeval, or nearly so, with the high-brow gravel of
the Thames, East-Hssex, and Canterbury sheets, the lower-terrace
beds of the Thames gravel formation are not, I venture to suggest,
coeval with the Elephant-gravels of Mr. Codrington, but are con-
Fig. 2.—.Theoretical Section connecting the Thames and Hampshire
Gravel Brows.
|
ES
8 :
Cire; = ‘ >
Se 3 3 =] 2 =
"S a a esl cS) tr ge oF 3
o 4&4 3 8 a S i a z =
a g = E Ea ae] | 2 FE oD
a a= ' 3 B 2 g 3 =
Ks Ss o ron: cat
SVEN WO AMS ay a0 Ja VE eee
fas let ul | b | Pak a
Vi |
# \\ ; | a IR —
RS nmr ag
Se 5 ShaPies z
os ee 4
Mr. Codrington’s inlet. The western extremity of the Weald.
1. Wealdclay. 2. Lower Greensand. 3. Gault, Malm Rock, and Upper Green-
sand. 4. Chalk. 5. The Lower Tertiaries. a. The sea-bottom on which
the high-brow gravel of the Thames and Hampshire sheets accumulated.
6. The sea-level of that period. c. The sea-bottom of the inlet wherein the
lower Hampshire marine gravels accumulated. d. The sea-level of that
period. The x X X markthe high brows of gravel of the London and
Hampshire areas. + The part over which the sharply broken flint accumu-
lations of Sir R. J. Murchison occur. indicates the foci of preglacial
upheaval. # indicates those of postglacial upheaval. (N.B. The Needle
Down should in the upper representation have been drawn free of Tertiaries
and near the sea surface.)
siderably anterior to them, and possess a well-known older and
somewhat different fauna, both mammalian and molluscan, though
of course posterior to the highest-brow gravels of either area. In
other words, the great slope of gravel which Mr. Codrington shows
as stretching from low levels (where it inosculates with the Elephant-
gravels of the valleys) up to brows where it is cut off by denudation
at elevations of 400 feet, represents, according to my view,,that long
postglacial period during which, over Surrey, Sussex, and Kent, those
extensive changes of land and water were proceeding which resulted
in the denudation of the Weald—the Selsey deposit (which I have
correlated with the retirement of the sea within the Wealden escarp-
ment) being covered by the lowest-level portion of the Hampshire
sheet.
Discussion.
Mr. Gopwiy-Atvsten thought that the author had done his theory
injustice in presenting only a portion of the Wealden area for con-
sideration. He remarked that phenomena similar to those of the
Weald were to be found in various parts of Western Europe. He
was glad to find that Mr. Searles Wood did not regard the escarp-
1870. ] W0OD—WEALD-VALLEY DENUDATION. 27
ments as representing marine cliffs; but he did not attach sufficient
weight to the absence of any material of marine origin at their base ;
so that there was no evidence of the presence of the sea within the
Wealden area. He differed wholly from the author as to the age of
the gravels ; for beneath the gravels were silty beds containing Ele-
phant-remains. These gravels he was inclined to refer to a glacial
period, as they contain blocks such as could have been transported
only by the agency of ice. The elephants found in the valley of
the Wey are of the species (H. primigenius) which also occurs in the
Selsey beds; and he believed both to be of glacial age. As to the theory
of the denudation of the Weald, he professed himself a convert to
the views of Messrs. Foster and Topley, and cited what was now
going on around Heligoland in illustration of denudation.
Mr. Wuitaker observed that the present absence of gravels along
parts of the valley of the Thames affords no proof of their not having
formerly existed. He pointed out the soft and friable nature of most
of the rocks of the Wealden, which would account for their absence
in the gravels. The only really hard rock was the Chert of the
Lower Greensand, which was abundant in the gravels of East
Kent. Angular flints occurred at the base of the chalk escarpment
wherever it had been carried back by denudation. The major valley
of the Weald had been spoken of ; but he denied that any such valley
existed; it was merely a series of numerous small valleys. He
could not conceive the rivers flowing against the dip of the strata,
as supposed by Mr. Wood. He did not agree in the view of the
denudation of the Weald being such an enormous affair, but thought
that it might be due to comparatively small causes.
The Present pointed out that beyond Southend there was a
section precisely similar to that of Grays. It was a mistake to suppose
that pebbles from the Wealden area did not occur in the Thames
gravels. He thought that much of the denudation of the Wealden
area might have taken place before the glacial period. The presence
of Tertiary pebbles in the Wealden area might readily be accounted
for by their presence at the edge of the escarpment.
Mr. Seartes V. Woop, Jun., in reply, justified himself for having
limited his observations to the northern part of the Weald, as it was
there only that it could be brought into juxtaposition with the Glacial
beds. He maintained that, under certain circumstances, no beaches
or marine beds were formed at the base of sea-cliffs. He pointed out
that in Postglacial gravels large blocks of rock were frequently
found, and protested against limiting all ice-transport to the glacial
period. He could not recognize the Selsey beds, with 150 living
species, some of southern character, and none extinct, as glacial.
The alleged softness of some of the Wealden rocks, when the great
excess both of the Lower-Greensand and Hastings-sand areas over
that of the Chalk was considered, did not at all remove the contra-
dictfon presented by the enormous preponderance of flint over sub-
cretaceous material in the East-Essex gravel. Like Mr. Austen, he
attributed the Wey gravels and the Selsey bed to nearly the same
period; but that was a late postglacial, instead of a glacial one.
28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 23,
NovemBer 23, 1870.
The following communications were read :—
1. On some pornts of Souru-Arrican Geotocy.—Part I.
By G. W. Stow, Esq.*
(Communicated by Prof. T. Rupert Jones, F.G-S.)
[ Abstract. ]
In this paper, which was illustrated by numerous sketches, sections,
tables, and specimens, observations were made on the stratification
of the Jurassic beds of Sunday’s and Zwartkop’s rivers, resulting
from researches made by Mr. Stow, with the view of determining
the exact position of the several species of fossils found at the expo-
sures on the cliffs of these rivers, and from this the sequence of the
various beds. He indicated the existence of at least nine separate
fossiliferous bands, pointing out the relative positions of the several
Trigonia-beds, Hamite-beds, Ammonite-beds, &c.
He next treated of the so-called Saliferous beds of the district, and
gave his reasons for regarding them as later in age than the Trigonia-
sandstones above alluded to, and therefore not equivalent to that
part of the series named “‘ Wood-beds” by Dr. Atherstone.
Other researches of the author related to the Tertiary beds, both
inland and on the coast. He distinguished three zones on the coast
later in date than the high-level shell limestones (Pliocene ?) of the
Grass Ridge and other parts of the interior. One of the coast-zones
he named the Akera-bed, from the prevalence of a delicate species
of that genus. Another zone was described as following the river-
valleys in the form of raised terraces, characterized by the presence
of a large Panopewa. The latest shell-banks have been thought to
be kitchen-middens ; but the author regarded them as shore-deposits
in place. The author concluded by tracing the probable climatal
and geographical changes in this region during geological times,
and indicated, as far as his material allowed, the probable migrations
of the Mollusca, especially of the Venericardia characterizing the
Pliocene Limestone.
Discussion.
Mr. J. Gwyn Jerrreys remarked that all the shells belonging to
the genus Akera which he had examined were shallow-water or lit-
toral shells.
Dr. Duncan remarked on one of the corals as being of a well-
known Crag form, the Balanophyllia calyculus.
Mr. Szartes Woop, Jun., remarked on the importance, if the con-
clusions of the author were sustained, of the older post-tertiary beds
denoting a warmer climate than the present, instead of, as in the
Northern Hemisphere, a colder.
* The publication of this paper is deferred.
1870. ] HULKE—REPTILIAN FOSSILS FROM GOZO. 29
2. Note on some Repritian Fosstzs from Gozo.
By J. W. Horxs, F.RB.S., F.G.S.
Turse fossils were collected by the late Captain Strickland, and for-
warded by Mrs. Strickland, for examination and description, to Mr.
Busk, who intrusted me with them for this purpose, informing me
at the same time that they came from Gozo, the Gauda of Strabo,
an island adjoining Malta, reputed miocene.
As one of the fossils indicates, I believe, a new crocodile, and
the other, if Gozo be really miocene, if the jaw actually came
thence, and if my determination should prove correct, shows the
survival of an Jchthyosaurus to a much later period than that of the
upper white chalk, the most recent formation in which any remains
of this genus have yet been found, they seemed to me worthy of
being brought under the notice of this Society.
IcHTHYOSAURUS GAUDENSIS.
The fossil which I venture to refer to the genus [chthyosaurus is
the symphysial part of a long slender mandible. The front end is
wanting; and the rami have also been broken off just behind the
symphysis. In its present mutilated state it measures 9 in. long,
1:2 transversely in front, and 2:1 at the posterior limit of the
symphysis. Its outer surface is trans-
versely gently convex, smooth, and finely Fig, 1—Tooth of Ichthyo-
wrinkled longitudinally. The upper sur- saurus gaudensis.
face presents a smooth narrow median
tract, in front greatly convex trans-
versely, behind slightly concave in the
same direction, mesially divided by the
symphysial suture, in which posteriorly
the splenial element is discernible. This ie
is bordered externally by a line of shallow Nacuealicie:
tooth-pits, separated by low transverse
ridges, the outer ends of which ascend a short distance on a low
parapet formed by the slightly higher outer edge of the dentary
bone. Most ofthe pits are empty; and their smooth surface shows
the absence of any firmer bond of union than the gum between the
teeth and the mandible.
The teeth are conical, the crown is slightly compressed, its trans-
verse section elliptical ; the fang is simple, of a bulbous figure, its
exterior is smooth, its base slightly contracted and rounded. The
principal tissue is a simple tubular dentine, in the crown covered
by a thick enamel, while in the fang it is enveloped by a stout
capsule of cementum. A pulp-cavity rises through the fang for some
distance into the crown. A minute plug of spar fills its upper end;
and its lower end encloses a little mass of osteo-dentine, which is
continuous, through the contracted basal end of the cavity, with the
external cementum.
30 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 23,
Twenty-one teeth occupy a space of 8 inches. The length of a
fang slightly exceeds °3”, the diameter (including the capsule) aver-
ages °3”, and that of the dentinal cylinder minus its investing cap-
sule -15”. The apices of all the crowns are broken off, so that the
entire length of the teeth is not determinable.
In their form and structure these teeth repeat so closely the
characters of those of the Kimmeridge Hnthekiodon as to suggest the
great probability of their both belonging to the same genus. My
note on Enthekiodon*, communicated last session, noticed the resem-
blance of its teeth and of the mode of their attachment to the jaw
to those of Ichthyosaurus ; but my material was too imperfect to
justify me in certainly referring it to that genus. J have now, how-
ever, indisputable evidence that it is a true [chthyosaurus; and this
being so, the similarity of the dental characters of this Gozo mandi-
ble to those of Hnthekiodon affords a strong presumption that it also
is Ichthyosaurian.
CROCODILUS GAUDENSIS.
The skull is in form elongated and subtriangular. Its sides con-
verge regularly from the posterior and outer angles of the quadrate
bones to the 8th tooth, counted fromm behind. From this they are
nearly parallel, to the 14th tooth, in front of which the snout is
slightly contracted where the premaxillo-maxillary suture crosses
its alveolar border. The end of the snout, including the external
nostril, is wanting.
The syncipital area is a nearly flat oblong, measuring transversely
along its posterior border 5-4, along its anterior border (a line con-
necting the anterior and outer angles of the postfrontal bones) 5”,
and from front to back 3-2. The entire surface of this area is sym-
metrically pitted. In its frontal part, which is hollow transversely —
and plane axially, the pits are grouped in lines diverging from the
axis of the skull, and there is a large remarkable pit in each pos-
terior angle of the area.
The supratemporal fosse are very large, and have an angulated
pentahedral shape. Their transverse diameter, slightly larger than
the others, is 18. The intervening parietal bone has a minimum
width under -1”.
The interorbital space is narrow, hollow transversely, plane axially,
and less strongly pitted than the syncipital area.
The orbits are large, their contour is subtriangular, incomplete
behind; they look directly upwards; and their long diameter is
directed from behind forwards and inwards. The outer, front, and
inner part of their margin is raised; and the front part is channelled
by two grooves, of which one descends longitudinally on the pre-
frontal bone, and the other along the junction of the prefrontal and
lachrymal bones.
The nasal bones posteriorly reach the level of a line joining the
anterior angles of the orbits, and, descending the snout in the form
* Quart. Journ. Geol. Soc. vol. xxvi. p. 172.
1870. | HULKE—REPTILIAN FOSSILS FROM GOZO. 31
of two narrow slips, they meet the premaxille opposite the interspace
between the 11th and 12th teeth, counted from behind. For some
distance above and below this spot, the widths of the nasals and of
the ascending slips of the premaxill are so nearly equal that the
junction of the two pairs of bones is inconspicuous and may easily
be overlooked.
The prefrontals form rather less than half of the inner border of
the orbit, and they are marked by the groove already described. The
lachrymals descend along the outer border of the nasals nearly as far
again as the prefrontals.
The upper surface of the snout has been flattened by pressure. It
is marked with a rather coarse longitudinal wrinkling. The borders
of the snout are even behind the 8th tooth, but in front of this the
prominence of the alveoli makes them slightly crenated.
The under surface of the skull has the common features of a croco-
dile’s. The mesial borders of the palatine and pterygoid bones meet
throughout their length. The posterior nares, wholly included
within the posterior border of the connate pterygoid als, look back-
wards. The transverse diameter of their opening slightly exceeds
the axial diameter. The pterygo-palatine foramina are long and
narrow, their inner border is nearly straight, and their outer border
is concave.
The occipital surface of the skull is nearly plane vertically, slightly
convex transversely above the foramen magnum, and external to
this slightly hollow.
The mandibular symphysis, with about 4” of both rami behind it,
and nearly as much in front of it, remains attached to the under sur-
face of the snout. The symphysis begins opposite the interspace
between the 7th and 8th maxillary teeth, counted from behind. The
splenial bones are included in it.
The teeth are subequal, conical, sharply pointed; when fully ex-
truded slightly retrocurved, unequally compressed laterally, the
outer surface more convex than the inner one, the compression
increasing towards the apex of the crown, and forming here a back
and front smooth edge. The hinder maxillary teeth are shorter, they
taper less, and are more compressed than those in front. The fang
is large, and it has a capacious, open pulp-cavity. The crown has a
thick coat of enamel, which on the outer side of the tooth is marked
by low longitudinal striz, widely set near the base, and closer and
finer near the apex; on the inner side it is extremely finely striated
or, rather, wrinkled.
A label affixed to the fossil before it came under my hands, and
when it was still nearly hidden in the matrix, showed that it had
been referred to Melitosaurus champsoides, Owen. I have compared
it with the type specimen of this species in the British Museum*, and
find that it agrees with this in the long mandibular symphysis, in the
narrowness of the ascending processes of the preemaxillz, and in the
* The terminal 13 inches of the maxilla and mandible of a large croco-
dilian.
32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 23,
manner of union of these with the nasal bones; but the teeth differ:
those of Melitosawrus champsoides (making allowance for the much
larger size of the individual) are stouter, much less sharply pointed,
and less tapering; their enamel marking has also a different cha-
racter, being much more finely wrinkled than in this Gozo crocodile.
In its elongated form and its regularly tapering outline (not sud-
denly contracted in front of the orbits as in the Indian gayial), in
the commencement of the nasal bones opposite the front borders of
the orbits, in the slenderness of these bones, and in their sensible
junction with the ascending processes of the preemaxille the skull of
the Gozo crocodile resembles that of the existing Rhynchosuchus
Schlegelii ; but it differs from it in several particulars, amongst
which are the crenation of the alveolar border of the distal halves of
the snout, the more oblong shape of the syncipital area, the larger
size and different shape of the supratemporal fosse, the raised mar-
gin of the orbit, and the more hollow interorbital space. I propose
for this Gozo crocodile the specific name of gaudensis.
Dimensions.
in.
From the posterior border of the syncipital area to the anterior ...... ..... 32
From ditto to the anterior border of the parietal bone ...........-......2-00+ 2:1
From ditto to the anterior limit of the frontal bone .................seeeeeeee 6-7
From ditto to the posterior limit of the prefrontal bone.................... «6 4-0
From ditto to the anterior limit of the prefrontal bone .....0........e.seseeeee 6:1
From ditto to the anterior limit of the lachrymal bone .............0cs++see0ee 71
From ditto to the anterior limit of the nasal bones ..........00-secseceseseceenes 14:6
From ditto to the posterior limit of ditto..........ccseessssesssccessecerererscenes 135
From ditto to the last maxillary tooth 020 .:-...--<ccosrscosscoos-cnn-we-cacasuseese 4-6
Breadth of syncipital area, its posterior border ...........sssseeeseccseceneeeens 5-4
Ditto; atstanterior’ DOL ebiie.sccseccaceodesch cece soc seneeeceascecbecsuccesse mereeeeter 5:0
Supratemporal foramina, axial diameter .............sscssseescrsceettcoceneseeees Use
IDMAIO), WAP VETESS) GUENGTEE soecosncooncencuodoooodosgoHonbooODOnGO sbaboAQDOACOCOdesnsOS 18
Interforaminal parietal septum, minimum width under ............s0ssseseesee 0-2
Orbits, distance between their inner borders.............cesecsersecccsscscccevence 1:0
Jositell, GUBMIN SEI Olf adridc sadnenguecoad-becoocQuoabodceucnocooconoDrosdbaAgasaDsecodoO9 2:3
SUERORTENE@ CHEMTNE NTE OH coonsogooscotoobonng}adanbadoanooDonDcHOsOFADCAoDADeAsOONNC 15
Breadth of skull at hindermost tooth.............ccsccsccsssccsscesssceeccecescerens 5:2
Ditto at 1LOth tooth from behind ...........ssscseesesseocescnvceseerceccereoee een
WDitibopn front ofplAt hi too bly een csmeeeesttem sellers teltectieaseasems sees ese eeeeeeeatd 1-6
IDermreilay ort (jal vanemaMlleNisy TOWNE) Gaodnne saggecod sodacnonen dosaneconteaonnapeSaqseoHtOs 16
Antero-posterior diameter of 10th maxillary tooth at the junction of the
GRO) Ha) TENE Gospooocpogan GacoooHdaqancconuoonEcoondodonancdodEncOOd. Boconqsqn60N60
Discussion.
Dr. Duncan suggested that the Ichthyosaurian fossil might be
derivative from some secondary rock. He mentioned that Dr. Leith
Adams had once sent him an Aspidiscus cristatus from the Hippu-
rite Limestone, which was stated to have come from Malta. To
account for this, he suggested that the Miocene of Malta might
have been supported on beds of Cretaceous age, and fossils from that
source might have become imbedded in the coral reefs of the later
date.
1870. | HULKE—REPTILIAN FOSSILS FROM GOZO. 33
Capt. Spratt expressed a doubt of the fossil having really come
from Gozo. He did not recognize the cretaceous-looking matrix
as belonging to any of the rocks of that island, with all of which
he was acquainted. The nearest approach to that kind of rock
was to be found in the lowest of the deposits near Cairo, which
were probably EKocene.
Prof. T. Rupert Jones suggested an examination of the Forami-
nifera in the matrix, with the view of determining its Secondary or
Tertiary age. He mentioned the occurrence of rolled nodules of
older rocks in beds of later age at Gozo.
Mr. Busx stated that a stone of similar character to the matrix
occurred in Malta, if not in Gozo, but probably in both.
Mr. Hurxz, in reply, observed that he had in his paper inten-
tionally left the stratigraphical part of the question untouched, and
confined himself to the paleeontological aspect of the remains.
3. On the Discovery of a “ Bonz Bep” in the Lowxst of the “ Lynton
Grey Bens,” Norra Devon. By F. Royston Farrpanx, M.D.
(Communicated by Prof. Duncan, M.B., F.R.S., Sec. G.S.)
[This paper is withdrawn by the author, by permission of the Council. |
VOL. XXVII.—PART I. D
34
DONATIONS
TO THE
LIBRARY OF THE GEOLOGICAL SOCIETY
From July 1st to September 30th, 1870.
I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.
American Academy of Arts and Sciences. Proceedings. Vol. viii.
pp. 1-186.
American Naturalist. Vol. iii. (Second copy.)
——. Vol.iv. Nos. 1, 2, 5-7.
W. W. Bailey—A Sketch of the Truckee and Humboldt Valleys,
ade
American Philosophical Society. Proceedings. Vol. xi. No. 82.
1869.
E. D. Cope.—Seventh Contribution to the Herpetology of Tropical
America, 147.
——. Synopsis of Extinct Mammalia of the Cave-formations in the
United States &., 171 (3 plates).
P. W. Sheafer.—Coal-borings in the Wilkesbarre Basin, 235.
Roscoe.—A letter from, respecting a supposed Laurentian Fossil,
237.
EK. D. Cope.—Second Addition to the History of the Fishes of the
Cretaceous of the United States, 240.
Atheneum (Journal). Nos. 2226-2239. July to September 1870.
Berlin. Monatsbericht der konigl.-preussischen Akademie der Wis-
senschaften zu Berlin. May 1870.
Rammelsberg.—Ueber einige die Geologie der Anden betreffende
Fragen, 326,
DONATIONS. 35
Berlin. Zeitschrift der deutschen geologischen Gesellschaft. Band
xxl. Heft, 2., 51870:
Grassi.—Ueber die Ausbriiche des Aetna im November und December
1868, 189.
H. Credner.—Die Kreide von New Jersey, 191 (1 plate).
J. Roth.—Ueber die Gleichzeitigkeit der Vulkane von Latium und
des Menschen und tber die palioethnologischen Funde in der
rémischen Campagna tberhaupt, 252.
Zeuschner.—Beschreibung neuer Arten oder eigenthiimlich ausgebil-
deter Versteinerungen, 265 (3 plates).
B. K. Emerson.—Die Liasmulde von Markoldendorf bei Hinbeck,
271 (8 plates).
J. Lemberg.—Ueber einige Umwandlungen finlandischer Feldspathe,
300. .
Zeuschner.—Einige Bemerkungen iiber die geognostische Karte von
Oberschlesien, bearbeitet von Herrn Ferdinand Roemer, 373.
P. Groth.—Ueber den Topas einiger Zinnerzlagerstatten, besonders
von Altenberg und Schlaggenwalde, sein Vorkommen und seine
Krystallformen, 381 (1 plate).
Daubrée.—Synthetische Versuche beziiglich der Meteoriten, Ver-
gleiche und Schlussfolgerungen, zu welchen diese Versuche fiihren,
415.
Boston. Proceedings of the Boston Society of Natural History.
Vol. xii. pp. 273-420, and Index.
—. ——. Vol. xu. pp. 1-224.
Calcutta. Asiatic Society of Bengal. Journal. New Series. Vol.
xxxix. Nos. 160 & 161.
——. -——. Proceedings. Nos. 4-6. April to June 1870.
Cambridge. Proceedings of the American Association for the
Advancement of Science. Seventeenth Meeting. Vol. xvii.
August 1868.
C. Whittlesey.—On the Hvyidence of the Antiquity of Man in the
United States, 268.
O. C. Marsh.—Description of a new species of Protichnites from the
Potsdam Sandstone of New York, 322.
On the Preservation of Colour in Fossils from Palzeozoie
Formations, 325.
C. A. White-—Announcement of the Existence of Cretaceous Rocks
in Guthrie County, Iowa, 326.
EK. W. Hilgard.—On the Geology of Lower Louisiana and the Rock-
salt Deposit of Petite Anse, 327.
C. A. White.—Observations on the Red Quartzite Boulders of
Western Iowa, and their original Ledges of Red Quartzite in
Towa, Dakota, and Minnesota, 340.
8. J. Wallace.—On the Old Lake Beds of the Prairie Region, 342.
Chemical News. Vol. xxi. No. 552. Vol. xxii. Nos. 553-566.
Chemical Society. Journal. Second Series. Vol. viii. June
September 1870. |
p2
36 DONATIONS.
Chicago Academy of Sciences. Transactions. Vol.i. Part 2. 1869.
J. W. Foster.—On the Antiquity of Man in North America, 227.
Colliery Guardian. Vol. xix. No. 495. Vol. xx. Nos. 496-509.
Copenhagen. Oversigt over det Kongelige danske Videnskabernes
Selskabs Forhandlinger. 1869, No. 3.
Darmstadt. Notizblatt des Vereins fir Erdkunde und verwandte
Wissenschaften zu Darmstadt, und des mittelrheinischen geolo-
gischen Vereins. Folge i. Heft 8.
R. Ludwig.—Versteinerungen im Stringocephalenkalke bei Wald-
Girmes, 29,
Ueber die Lagerungsverhiltnisse der Dyasformation bei Bu-
dingen in Oberhessen, 174.
——. Ueber die Lagerungsverhaltnisse der Dyasformation bei Frau-
Nauses im Odenwalde, 175.
English Mechanic. Vol. xi. Nos. 276-284.
Essex Institute. Bulletin. Vol.i. 1869.
C. M. Tracy.—Notice of a singlar Erratic in Lynn, Mass,, known by
the name of “ Phaeton Rock,” 59.
Act of Incorporation, Constitution, and By-Laws, and Cata-
logue of the Officers and Members.
An Historical Notice of the, with the Act of Incorporation,
Constitution, and By-Laws, and Lists of Members. 1866.
——. Proceedings. Vol. iv. Part 1. 1868.
Florence. Bollettino del Reale Comitato Geologico d'Italia. Nos.
6-8. June to August 1870.
G. Grattarola ed A. Alessandri—Cenni intorno alla distribuzione del
terreno postpliocenico nelle valli all’ Est di Firenze, 149.
EK. Suess.—Intorno al Rothliegende nella Val Trompia, 155.
H. Wolf.—I giacimento zolfifero di Tufo ed Altavilla, 160.
T. Caruel.—Osservazioni sul genere di Cicadacee fossili Rawmeria,
e descrizione di una specie nuova, 181.
Abdullah Bey.—Remarques géologiques sur le calcaire dévonien du
Bosphore, 187.
H. Gerlach.Sulla Geologia del versante meridionale delle Alpi
Pennine, 190.
E. Suess.—I rappresentanti dei terreni Carbonifero e Permiano nelle
Alpi, 207.
Geological Magazine. Vol. vii. Nos. 7-9. July to September 1870.
W. Carruthers.—On the Petrified Forest near Cairo, 306 (1 plate).
G. H. Kinahan.—Features of Devon, Cornwall, and Galway com-
pared, 310.
D. Forbes.—On Volcanos, 314.
EK. Hodgson.—The Granite-drift of Furness, 328 (1 plate).
D. Mackintosh.—On the Dispersion of Shapfell Boulders and Origin
of Boulder-clay, 349.
J. Opler nen and affinities of Dicranograptus, 353 (1
plate).
DONATIONS. 837
Geological Magazine. Vol. vii. Nos. 7-9 (continued).
T. Davidson.—On Italian Tertiary Brachiopoda, 359, 399 (4 plates).
E. Ray Lankester.—On a new Cephalaspis dissoverbd in America ;’on
Macharacanthus, and Scaphaspis Kneriw, 397.
A. Marston.—On the Transition Beds between the Devonian and
Silurian Rocks, 408.
E. Ray Lankester—On a new large Terebratula occurring in Kast
Anglia, 410,
R. H. Scott.—Descriptive Catalogue of the Fossil Mammalia found
in Ireland, 413.
Pratt.—Reply to M. Delaunay’s objections to the late Mr. Hopkins’s
method of determining the thickness of the Earth’s Crust, 421.
‘Records of the Geological Survey of India,’ noticed, 339, 379, 427.
T. R. Jones’s ‘The Primeval Rivers of Britain,’ noticed, 371.
P. M. Duncan and H. M. Jenkins ‘On Paleocoryne, a new genus of
Hydrozoa, noticed, 376.
O. C. Marsh’s ‘New Fossil Reptiles and Birds from the United
States,’ noticed, 376.
F. Roemer ‘On a new Fossil Snake, Python euboicus,’ noticed, 424.
E. D. Cope ‘On some new American Fossil Reptiles,’ noticed, 426.
O. C. Marsh ‘On a new Eocene Gayial,’ noticed, 427.
Seeley’s ‘ Ornithosauria,’ reviewed, 341.
‘The Explorer’s Test Case,’ reviewed, 381.
Hall’s ‘ Mineralogist’s Directory,’ reviewed, 382.
Catlin’s ‘ Lifted and Subsided Rocks,’ reviewed, 383.
“Report of the Rugby School Natural-History Society for 1869,’
reviewed, 429.
C. E. de Rance’s ‘Geology of the country between Liverpool and
Southport,’ reviewed, 480.
Reports and Proceedings of Societies, 343, 386, 481.
Correspondence, 347, 394, 440.
Miscellaneous, 348, 395, 444.
Harlem. Archives Néerlandaises des Sciences Exactes et Natu-
relles publiées par la Société Hollandaise des Sciences 4 Harlem.
Tome y. Livraisons 1-3. 1870.
H. H. H. van Zouteveen.—La forét pétrifiée du Caire, les collines de
tessons de poterie de la Basse-Egypte et la premiére cataracte du
Nil, 238.
Iron and Coal Trades Review. Vol. iv. Nos. 124-135. July to
September 1870.
Linnean Society of London. Journal. Botany. Vol. xi. Nos. 54:
& 55.
——. Proceedings. Session 1869-70.
——. Transactions. Vol, xxvi. Part 4.
W. C. Williamson.—Contributions towards the History of Zamia
Gigas, 663.
W. Carruthers.—On Fossil Cycadean Stems from the Secondary
Rocks of Britain, 675.
a Volmeseavanen bares elias (2.
38 DONATIONS.
London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xl. Nos. 264-266. From Dr. W. Francis, F.G.S.
J. Ball—On the Cause of the Descent of Glaciers, 1.
Archdeacon Pratt——Reply to M. Delaunay’s objection to the late
Mr. Hopkins’s Method of determining the Thickness of the Earth’s
Crust by the Precession and Nutation of the Earth’s Axis, 10.
J. Croll_—On the Cause of the Motion of Glaciers, 153.
Longman’s Notes on Books. Vol. iv. No. 62. August 1870.
Milan. Atti della Societé Italiana di Scienze Naturali. Vol. xii.
Fascicoli 3 & 4. February and March 1870.
Proceedings of the Geological Section in Catania, 456.
Escursione ad Aci-Castello, ai Faraglioni e ad Aci-Reale del 24
agosto 1869, 492.
Ascensione dell’ Ktna del 27 e 28 detto, 495.
Aradas.—Un abozzo del Panorama etneo. Discorso d’apertura della
Riunione, 499.
Brevissimo sunto della Conchigliologia etnea, 535.
Descrizione di una nuova specie del genere Triforis di Des-
hayes, 547.
Renoit e Aradas.—Nota su aleune conchiglie di Sicilia pubblicate
come nuove dal prof. Carmelo Maravigna, 599.
Boe ae la posizione stratigrafica del Clypeaster altus,
k., 657.
Foti.—Succinta descrizione della geologia di Barcellona e territory]
circonvicini, 661.
Monthly Microscopical Journal. Vol. iii. Nos. 19-21. July to
September 1870.
8. Allport.—The Microscopical Examination of Rocks and Minerals,
Moscow. Bulletin de la Société Impériale des Naturalistes de Mos-
cou. Année 1869. No.4. 1870.
P. Kropotkin.—Geognostisches tiber den Kreis Mjeschtschowsk im
Gouvernement Kaluga nebst palaontologischem Beitrag von H.
Trautschold, 215 (1 plate).
R. Hermann.—Ueber die Zusammensetzung des Lawrowits, sowie
uber Vanadiolith, ein neues Mineral, 234.
Ueber die wahrscheinliche Identitat von Laxmannit und
Vauquelinit, sowie titber Phosphorchromit, ein neues Mineral, 240.
Nature (Journal). Vol. ii. Nos. 34-48. June to September 1870.
H. P. Malet.—The Interior of the Earth, 141.
R. C. Hart.—Geology and the Chatham Dockyard, 148.
W. Boyd Dawkins.—Fossil Mammals of North America, 282.
D. Forbes.—On Volcanoes, 283, 336. _
A. Geikie.—The Ice-age in Switzerland, 310.
A. H. Green.—Volcanic Agency v. Denudation, 375.
W. Luscombe.—Geology of Devonshire, 376.
J. 8. Newberry.—On Ancient Lakes of Western America, their
Deposits and Drainage, 385.
G. E. De Rance.—Notes on the Geology of the County around
Liverpool, 391.
J. P. Earwaker.—Geological Discoveries in Liverpool, 397.
DONATIONS. 39
New York. Annals of the Lyceum of Natural History. Vol. ix.
pp- 141-812.
J. S. Newberry.—On the Surface-geology of the Basin of the Great
Lakes and the Valley of the Mississippi.
Northumberland and Durham. Natural-History Transactions.
Vol. i. Part 2. 1870.
T. Atthey.—On the occurrence of the Palatal Teeth of a Fish
belonging to the genus Chmaxodus, M’Coy, in the Low Main
Shale of Newsham, 306.
A. Hancock.—On a new Labyrinthodont Amphibian from the
Northumberland Coal-field, and on the occurrence in the same
locality of Anthracosaurus Russelli, 310.
and T. Atthey.—Note on Anthracosaurus, 319.
. On some curious Fossil Fungi from the Black Shale
of the Northumberland Coal-field, 321 (2 plates).
. On the generic identity of Climaxodus and Janassa,
Fossil Fishes related to the Rays, 330 (1 plate).
A. Hancock and R. Howse.—On Janassa bituminosa, Schlotheim,
from the Marl-Slate of Midderidge, Durham, 339 (2 plates).
J. W. Kirkby.—Note on the “ Geology” of Messrs. Baker and Tate’s
New Flora of Northumberland and Durham, 357.
W. C. Trevelyan.—Note on the occurrence of the Trunk of an Oak
in the Boulder-clay, 382.
Paris. Bulletin de la Société Géologique de France. Deuxieme
Serie. Tome xxvi. No.7. 1869.
Belgrand.—L’age des tourbes dans le bassin de la Seine, 897 (1 plate).
Roueeos (Vabbé).—Sur les silex des dépdts miocénes de Thenay,
901.
Ponzi.—Le volcanisme romain, 903.
Tardy.—Note sur le Vivarais, 912.
Daubrée.—Sur lexistence de gisements de bauxite dans les départe-
ments de l’Hérault et de l’Ariége, 915.
ee: derniéres travaux sur le dyas et le trias de Russie,
Tardy.—Notes sur quelques éboulements, 924.
Ebray.—Assimilation de la protogéne des Alpes au porphyre grani-
toide du Beaujolais, 927.
Terquem et Jourdy.—Sur le terrain bathonien de la Moselle et de la
Meuse, 947.
Tournouér.—Sur des Nummulites et une nouvelle espéce d’Echinide
trouvées dans le miocéne inférieur des environs de Paris, 974.
Sur l’age géologique des mollasses de Agenais, 983.
Note additionnelle, 1020.
Gruner.—Sur un vieux bois d’étai de la mine de Littry (Calvados),
1023.
Delesse.—Lithologie des mers de l’ancien monde, 1025.
Ebray.—Sujets d’études dans le département de la Haute-Loire,
1021.
Tome xxvii. Nos. 1-3. 1870.
Le Hon.—Notes sur les Aptychus, 10.
Ey de l’existence du terrain houiller dans |’Ariéze,
4,
40 DONATIONS,
Paris. Bulletin de la Soci¢té Géologique de France. Deuxiéme
Série. Tome xxvii. Nos. 1-3 (continued).
Arnaud.—Observations géographiques sur la craie du Sud-Ouest,
18.
Desor.—Sur les terrains de transport de la vallée de la Durance,
Coquand.—Apercu géologique sur la vallée d’Ossau(Basses-Pyrénées),
43
Hébert.—Observations sur la communication précédente, 71.
Coquand.—Nouvelles considérations sur les calcaires jurassiques 4
Diceras du midi de la France, 73.
Hébert.—Examen de quelques points de la géologie de Ja France
méridionale, 107.
Stoppani.—Sur la genése des laves, 137, 161.
Planté (Gaston):—Sur les lignites inferieurs de l’argile plastique du
Bassin Parisien, 204 (1 plate).
De Tchihatcheff-—Sur la paléontologie de l’Asie centrale, 218.
De Keyserling.—Sur l’envahissement du golfe de Reval par les glaces
flottantes, 228.
J. Martin.—Les glaciers du Morvan, 225.
Cazalis de Fondouce.—Sur la rencontre de quelques ossements
fossiles dans les environs de Durfort (Gard), 264.
Pouech.—Sur les poudingues tertiaires dits de Palassou dans le dé-
partement de l’Ariége, 267.
Tombeck.—Sur le lias de la Haute Marne, 286, 289.
Ern. Favre.—Sur la craie de la Galicie Orientale, 291.
Eug. Deslongchamps.—Sur les Téléosauriens recueillis en Normandie,
299 (7 plates).
Tardy.—Sur un silex taillé du Cantal, 358.
Marcou.—Sur les anciens glaciers de l’Auvergne, 361.
Hébert.—Sur les grés infraliasiques de Scanie (Suéde), 366.
Oustalet.—Sur les couches 4 Meletta situées & Froide-fontaine (Haut-
Rhin), 380.
E, Sauvage.—Sur les poissons de Froide-fontaine, 397 (2 plates).
Indes.—Sur la formation des tufs des environs de Rome, 410.
Dieulafait.—Position de l’Ostrea Coulont dans le néocomien du sud-
est de la France, 431.
Guillier—Profils geologiques des routes du département de la
Sarthe, 435.
Bayan.—Sur les terrains tertiaires de la Vénitie, 444.
Comptes Rendus hebdomadaires des Séances de l’Académie
des Sciences. Premier Semestre 1870. Tomelxx. Nos, 15-26.
Backer.—Tremblements de terre et explosions volcaniques constatés
dans les Indes néerlandaises, depuis le commencement du xvi*
siécle jusqu’a nos jours, 878.
Bécamp.—Sur les microzymas géologiques de diverses origines, 914.
Richard.—Découverte d’un atelier d’instruments préhistoriques en
Palestine, 949.
Pisanii—Sur les minéraux trouvés dans la mine de cuivre du cap
Garonne (Var), 1001.
Belgrand.—Le bassin Parisien aux Ages antéhistoriques, 1080.
Raoult.—Composition du gaz de la fontaine ardente de Saint-Bar-
thélemy (Isére), 1095.
Vézian.—Sur le systéme des filons du Hundsriick, 1125.
Botella.—Sur deux faits contemporains de soulévement, 1141.
DONATIONS. 4l
Paris. Comptes Rendus hebdomadaires des Séances de l’Académie
des Sciences. Premier Semestre 1870. Tome lxx. Nos. 15—26
(continued).
Elie de’ Beaumont.—Remarques relatives 4 la précédente communi-
cation, 1142.
Renault.—Mémoire sur Vorganisation de rameaux silicifiés apparte-
nant probablement & un Sphenophyllum, 1158.
Béchamp.—Note relative aux expériences quil se propose d’entre-
pond concernant l’existence des microzymas dans les roches,
64. ;
Scheurer—Kestner.—De l’action de l’acide chlorhydrique sur l’osséine.
Nouvelles recherches sur le dosage de l’osséine dans les ossements
fossiles, 1179.
Montagna.—Sur existence de restes organiques dans des roches con-
sidérées comme ayant une origine ignée, 1415.
Deuxieme Semestre 1870. Tome lxxi. Nos. 1-4.
Elie de Beaumont.—Note sur les roches qu’on a rencontrées dans le
creusement du tunnel des Alpes. occidentales, entre Modane et
Bardonnéche, 8.
Vélain.—Sur la position des calcaires 4 Terebratula janitor, dans les
Basses-Alpes, 85.
Faye.—Remarques sur quelques particularités du sol des Landes de
Gascogne, 245.
Dieulafait.—Note sur les calcaires 4 Terebratula diphya dans les Alpes
frangaises, de Grenoble 4 la Méditerranée, 282.
Pissis.—Systéme de montagnes et terrains du désert d’Atacama, 285.
Garrigou et Chasteigner—Contemporanéité de Vhomme avec le grand
ours des cavernes et le renne dans la caverne de Gargas (Hautes-
Pyrénées), 288,
Plymouth. Annual Report and Transactions of the Plymouth Insti-
tution and Devon and Cornwall Natural-History Society. Vol. iv.
Part 1. 1866-70.
G. W. Ormerod.—On Common Salt, 21.
Quarterly Journal of Science. No. 27. July 1870.
H. M. Jenkins.—The Rate of Geological Change, 322.
Quekett Microscopical Club. Journal. No. 11. July 1870.
——. Fifth Report; and List of Members. July 1870.
Royal Geographical Society. Proceedings. Vol. xiv. No. 2.
H. Cook.—Notes on the Climate and Geology of Abyssinia, with
Table of Heights, 158.
Royal Society. Proceedings. Vol. xviii. Nos. 120-122.
St. Petersburg. Bulletin de Académie Impériale des Sciences de
St. Pétersbourg. Tome xiv. Nos. 4-6.
J. F. Brandt.—Sur le poil du Rhinoceros tichorinus, 353.
G. v. Helmersen.—Notice sur Ak-tau et Kara-tau, montagnes dans
FS ineeuils de Mangyschlak, céte orientale de.la mer Caspienne,
492 DONATIONS.
St. Petersburg. Mémoires de |’Académie Imperiale des Sciences de
St. Pétersbourg. 7™° Série. Tome xiv. Nos. 8 & 9.
Tome xv. Nos. 1-4.
W. Besobrasof.—Revenus des Mines. Premiére partie, No. 4.
Society of Arts. Journal. 116th Session. Nos. 918-932.
Strasbourg. Bulletin de la Société des Sciences Naturelles de Stras-
bourg. 2° Année. Nos. 8-10. 1869.
C. Grad.—Observations sur la constitution et la mouvement des
Glaciers, 130.
Student and Intellectual Observer. New Series. Vol.i. No. 3.
Stuttgart. Jahreshefte des Vereins fir vaterlandische Naturkunde
in Wiirttembere. Band xxv. Hefte 2 & 3.
H. H. Bach.—Beitrag zur Kenntniss der geologischen Verhaltnisse
der Hiszeit, 113 (1 plate).
G. Werner. —Zusammenstellung der bis jetzt in Wurttemberg aufge-
fundenen Mineralien, 127.
E. Bessels.—Ueber fossile Selachiereier, 152 (1 plate).
M. Bauer.—Ueber einige altere Versuche auf Stembanlen 204.
—_—_—_
'e
Vienna. Anzeiger der k.-k. Akademie der Wissenschaften in Wien.
1870. Nos. 16-20.
Verhandlungen der k.-k. geologischen Reichsanstalt. 1870.
Nos. 9 & 11.
J. Haast.—Notizen aus Neuseeland, 157.
O. Boettger.— Revision der tertiaéren Land- und Susswasser- Versteine-
rungen des nordlichen Bohmens, 158.
G. Tschermak.—Ueber den Trinkerit, ein neues Harz, von Carpano
in Istrien, 158.
H. Abich—Die Reihen-Vulcan-Gruppe des Abul und Samsar auf
dem kaukasischen Isthmus, 159.
E. v. Mojsisovics.—Ueber das Vorkommen der sogenannten “ Augen-
steine ” in den Siidalpen, 159.
K. Peters.—Ueber den Plattengneiss, den Sauerling und einen feld-
spathfiihrenden Kalkstein von Stainz ; die Machtigkeit des Voits-
berger Lignits, 200.
C. W. Giimbel.—Ueber Nulliporenkalk und Coccolithen, 201.
E. v. Jahn.—Idrianer Korallenerz, Kainit von Kalusz, 205.
F. J. Kautmann.—Seekreide, Scheibkreide und die sogenannten
dichten Kalksteine sind krystallinische Niederschlage, 208.
J. Hafner.—Der Marmor von Schlanders, 207.
F. Foetterle—Die Umgebung von Baziasch, 209.
. Die Gegend zwischen Bukarest und der siebenbiirgischen
Grenze, 209.
D. Stur.—Das Gebiet zwischen Bebrina und Grabovce in der Mili-,
targrenze, 210.
H. Wolf.—Die Umgebung von Peterwardein und Karlowitz, 213.
Die geologischen Verhaltnisse des Titler Bataillons-Grenz-
gebietes, 215.
G. Stache.—Die krystallinischen Schiefergesteine im Zillerthale i in
Tyrol, 216.
Ee siienthtin an
2
DONATIONS. 43
Washington. Smithsonian Miscellaneous Collections. Vols. viii.
and ix. 8vo. Washington, 1869.
Smithsonian Contributions to Knowledge. Vol. xvi. 4to.
Washington, 1870.
Wellington. Transactions and Proceedings of the New-Zealand
Institute. 1869, Vol. ii. 1870.
R. Pharazyn.—Remarks on the Coast-line between Kai Iwi and
Waitotara, on the west coast of the Province of Wellington, 158.
J. ©. Crawford.—On Alluvial Gold in the Province of Wellington,
160.
Hutton.—On the Geology of the North Head of Manukau Harbour,
161.
_ J. Stewart.—Description of Lava-caves at the “Three Kings,” near
Auckland, 162.
J. Buchanan.—On the Wanganui Beds (Upper Tertiaries), 163.
C. Traill.—On the Tertiary Series of Oamaru and Moeraki, 166.
R. Gillies.—Account of a visit to a Hot Spring called “ Te Puia,”
near Wangape Lake, Central Waikato, Auckland, in August 1868,
169.
Notes on the Geology of the outlying islands of New Zealand; with
extracts from official Reports. Communicated by J. Hector, M.D.,
176.
J. Haast.—Notes on a Collection of Saurian remains from the Wai-
para River, Canterbury, in the possession of T. H. C. Hood, Esgq.,
186.
II. PERIODICALS PURCHASED FOR THE LIBRARY.
Annals and Magazine of Natural History. Fourth Series. Vol. vi.
Nos. 31-33. July to September 1870.
A. Hancock and T. Atthey.—Description of a Labyrinthodont Am-
phibian, a new generic form, obtained in the Coal-shale at News-
ham, near Neweastle-upon-Tyne, 56 (1 plate).
H. G. Seeley.—Remarks on Prof. Owen’s Monograph on Dimorpho-
don, 129.
Paleontographica: herausgegeben yon Dr. W. Dunker und Dr. K.
A. Zittel. Vol. xvii. Part 5.
O. Fraas.—Dzplobune bavaricum, 177 (1 plate).
W. Waagen.—Ueber die Ansatzstelle der Haftmuskeln beim Nautilus
und den Ammoniten, 185 (2 plates).
K. A. Zittel—Ueber den Brachial-Apparat bei einigen jurassischen
Terebratuliden und iiber eine neue Brachiopodengattung Dimeredla,
211 (1 plate).
44 DONATIONS.
Paleontographica: herausgegeben von Dr. W. Dunker und Dr. K.
A. Zittel. Vol. xvii. Part 5 (continwed).
H. v. Meyer.—Ueber Titanomys visenoviensis und andere Nager aus
der Braunkohle von Rott, 225 (1 plate).
O. Schilling.—Ueber eine Asteride aus dem Coralrag des Lindener
Berges bei Hannover, 233 (1 plate).
: Supplement. Zweite Abtheilung. 8vo; with Atlas,
folio. Cassel, 1870.
K. A. Zittel—Fauna der altern Cephalopodenfiihrenden Tithonbil-
dungen.
III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.
Achiardi, A. @. Sopra alcuni Minerali dell’ Elba. 8vo. Pisa,
1870.
——. Sopra alcuni Minerali e Rocce del Pert. Lettera di A.
d’Achiardi a Carlo Regnoli. 8yvo. Pisa, 1870.
Adams, A. L. Notes of a Naturalist in the Nile Valley and Malta.
8vo. 1870.
Agassiz, Z. Address delivered on the Centennial Anniversary of
the Birth of Alexander von Humboldt. S8vo. Boston, 1869.
Anderson, B. Narrative of a Journey to Musardu. 8vo. New
York, 1870.
Barrande, J. Défense des Colonies. IV. 8vo. Prague et Paris,
1870.
Beckles, S. H. The Sea-beach Question. 12mo. 1870.
Bell, A. Catalogue des Mollusques Fossiles des Marnes Bleues de
Biot, prés Antibes (Alpes-Maritimes). 8vo. Paris, 1870.
On some new or little-known Shells &c. of the Crag For-
mation. 8vo. 1870.
Bowerbank, J.S. On the Sea-beach Question. (Reprinted from the
‘ Hastings and St. Leonards News.”) 1870.
Caruana, A. A. Enumeratio Ordinata Molluscorum Gaulo-Meli-
tensium of the late Mr. G. Mamo. 8vo. Malta, 1870.
Dall, W. H. Observations on the Geology of Alaska. Large 8vo,
with Map. 1865-68.
Desguin, P, Etude sur le Maroc. 8vo. Anvers, 1870.
DONATIONS. 45
Deslongchamps, Eugene. Notes Paléontologiques. 1° volume. 8vo.
Caen et Paris, 1863-1869.
Gould, A. A. Report of the Invertebrata of Massachusetts. 8vo.
Boston, 1870. Presented by W. D. Binney, Esq.
Hall, J. Natural History of New York—Paleontology. Vol. iv.
Part 6. 4to. 1867.
Hesse. Geologische Specialkarte des Grossherzogthums Hessen und
der angrenzenden Landesgebiete. Section Alsfeld, von Rudolph
Ludwig. Folio. Darmstadt, 1869, with explanation. rom the
Geological Society of the Middle Rhine.
Hill, T, The Annual Address before the Harvard Natural History
Society. S8vo. Cambridge, 1853.
Hoffmann, C. K., und Weyenbergh, H., jr. Die Osteologie und
Myologie von Scewrus vulgaris, L. 4to. Haarlem, 1870.
Hull, H. M. Tasmania in 1870; or Hints to Emigrants, Lane
Settlers, and Capitalists. 12mo. Hobart Town, 1870.
Hunt, T. S. Notes on Iron and Iron Ores. 8vo. 1870.
Jones, T. R. On the Primeval Rivers of Britain. 8vo. 1869.
Lapham, F, A. A New Geological Map of Wisconsin. 1869.
Lea, Issac. Index to Vol. XII. and Supplementary Index to Vols. I.
to XI. of Observations on the Genus Unio. 4to. Philadelphia,
1869.
Lobley, J. Z. Mount Vesuvius: a Descriptive, Historical, and Geo-
logical Account of the Volcano. 8vo. 1868,
Marcou, J. Les derniers travaux sur les Dyas et Trias de Russie.
8vo. Paris, 1869.
Notes pour servir 4 V’histoire des anciens glaciers de l’Au-
vergne. 8vo. Paris, 1867.
Notes pour servir a histoire des anciens glaciers de l’Au-
vergne. 8vo. Paris, 1870.
Notes sur une Météorite tombée le 11 Juillet 1868, 4 Lavaux,
pros Ornans (Doubs). 8vo. Paris, 1868.
. Notice Biographique sur M. Auguste Dollfus-Gros. 8vo.
Paris, 1869.
——. Une Ascension dans les Montagnes Rocheuses. S8vo. Paris,
1867.
46 DONATIONS.
Minnesota. Annual Reports of the Minnesota Historical Society of
the Legislature of Minnesota for the years 1868 and 1869. From
the Government of Minnesota.
Charter, Constitution, and By-Laws of the Minnesota His-
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Minnesota. ~
, its Progress and Capabilities; being the second Annual
Report of the Commissioner of Statistics, for the years 1860 and
1861. 8vo. St. Paul, 1862. From the Government of Minne-
sota.
Statistics of Minnesota for 1869. S8vo. St. Paul, 1870.
From the Government of Minnesota.
New Zealand. Reports of the Geological Survey of New Zealand.
1865-69. From the Geological Survey of New Zealand.
Oustalet et Sauvage, MM. Notes sur les Schistes 4 Meletta de
Froide-fontaine. 8vo. Paris, 1870.
Packard, A. S. Record of American Entomology for the year 1868.
8vo. Salem, 1869.
Parrish, R. A., jun. Details of an unpaid Claim on France for
24,000,000 frances, guaranteed by the Parole of Napoleon III.
8vo. Philadelphia, 1869.
Perry, J. B. Queries on the Red Sandstone of Vermont, and its
Relations to other Rocks. 8vo. Boston, 1868.
Report. First Annual Report of the Trustees of the Peabody
Academy of Science, January 1869. 8vo. Salem, 1869. Pre-
sented by the Peabody Academy of Scence.
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York.
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Report of the Commissioner of Agriculture for the year 1867. 8vo.
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~ Report of the Commissioner of Patents for the year 1867. 4 vols.
From the Patent Office, Washington.
“ Research.” Statement of a recently claimed discovery in Natural
Science. S8vo. Melbourne, 1870.
Reuss, A. HE. Die fossilen Mollusken des Tertiir-Beckens von
Wien, von Dr. Moriz Hornes. Band II. Nr. 9 and 10. Bivalven.
Folio. Wien, 1870.
. Paliontologische Studien tber die alteren Tertiirschichten
der Alpen. IL. Abtheilung. 4to. Wien, 1869.
Ueber tertiire Bryozoen von Kischenew in Bessarabien. 8vo.
Vienna, 1869.
Safford, J. M. Geology of Tennessee. S8vo. 1869.
Sandberger, F. Ueber die bisherigen Funde im Wiirzburger Pfahl-
bau. 8vo. Wirzburg, 1870.
Smithsonian Institution. Annual Report of the Board of Regents.
8vo. Washington, 1869. From the Smithsonian Institution.
Spratt, T. A. B. On the Evidence of the Rapid Silting in Progress
~ at Port Said, the entrance to the Suez Canal. S8vo. 1870.
Streeter, G. LZ. An Account of the Newspapers and other Periodicals
published in Salem from 1768 to 1856. 12mo. Salem, 1856.
Suringar, W. F. R. Alge Japonice Musei Botanici Lugduno-
Batavi. 4to. MHarlemi, 1870.
Trutat et Cartailhac, MM. Matériaux pour Vhistoire primitive et
naturelle de PHomme. 6° Année, Nos. 4-6. 8vo. Paris,
1870.
Ulrich, G. H. F. Contributions to the Mineralogy of Victoria. 8vo.
Melbourne, 1870.
Vennor, H.G. Report on the Geology of Hastings County, Ontario.
8vo. Montreal, 1870. Presented by Edward Hartley, Esq.,
BGS.
Victoria. Mineral Statistics for the year 1869 (8 copies). From the
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Reports of the Mining Surveyors and Registrars. Quarter
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Victoria.
Whattlesey, C. A Report of Explorations in the Mineral Regions
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Cleveland, 1866.
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Winkler, T.C. Description d@’un nouvel exemplaire de Pterodactylus
mucronyx du Musée Teyler. Large 8vo. Harlem, 1870. :
Wright, T. The Correlation of the Jurassic Rocks of the Céte-d’Or —
and the Cotteswold Hills. 8vo. 1869.
IVY. BOOKS PURCHASED FOR THE LIBRARY.
Beaumont, L. E. de. Legons de Géologie Pratique. Tome ii. 8vyo,
Paris, 1869.
Dechen, H. von. Erlaiuterungen zur geologischen Karte der Rhein-
provinz und der Provinz Westphalen, sowie einiger angrenzenden
Gegenden. Bandi. 8vo. Bonn, 1870.
Hamy, E.-T. Précis de Paléontologie Humaine. 8yo. Paris,
1870,
Lennier, G. Etudes Géologiques et Paléontologiques sur ’Embou-
chure de la Seine et les Falaises de la Haute-Normandie. 4to.
Havre.
Milne-Edwards, A. Recherches anatomiques et Paléontologiques
sur les Oiseaux Fossiles de la France. Livr. 31-34. 1870.
Omboni, G. Geologia dell’ Italia. Small 8vo. Milano, 1869.
Paléontologie Francaise. Terrain Crétacé. Vol. VIII. Livr. 25.
Zoophytes, par M. de Fromentel. Texte, feuilles 22 4 24; Atlas,
planches 85 a 96.
Percy, J. The Metallurgy of Lead, including Desilverization and
Cupellation. 8yo, London, 1870.
THE
QUARTERLY JOURNAL
OF
THE GEOLOGICAL SOCIETY OF LONDON.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
Decremser 7, 1870.
The Rev. J. W. Todd, D.D., Tudor House, Sydenham, S.E.; The
Hon. Henry Ayers, Adelaide, South Australia; R. W. Peregrine
Birch, Esq., C.E., Palace Chambers, Westminster, S.W.; Alfred
Stair, Esq., 4 Surinam Terrace, Stratford, Essex; H. Rivett Carnac,
Esq., of Simla, E. Indies; Thomas Davies, Esq., 47 Rutland Road,
South Hackney, E.; the Rev. 8. H. Cooke, Northbourne Rectory,
Deal; J. 8S. Courtney, Esq., Penzance; John Johnson, Esq., C.K.,
Chilton Hall, Ferry Hill, Durham; the Rev. R. H. Morris, M.A.,
Principal of the Training College for South Wales and Monmouth-
shire, Caermarthen; and Joseph Drew, Ksq., J.P., Belgrave Ter-
race, Weymouth, were elected Fellows of the Society.
The following communications were read :—
1. Remarks on some SPECIMENS from South AFRICA.
By Grorcr Grey, M.D., of Cradock, Cape Colony.
(Communicated, with Notes, by Professor T. Rupert Jones, F.G.S.)
[ Abstract. |
Specmens.—§ A. From the Karoo Formation.—l. Rippled sand-
stone; 2. Shale with EHstherie, near Cradock ; 3. Skulls and bones
of two or more species of Dicynodon ; 4. Water-worn slab of sand-
stone, containing the skull of a Labyrinthodont (?); 5. Block of coal,
from the north-east margin of the Stormberg range; 6. Fossil
plants from the same locality, comprising Lepidodendron*, Sigil-
* [Dr. Rubidge ‘also refers to Lepidodendron as a Karoo fossil plant, in Quart:
Journ. Geol. Soc. vol. xii. p. 237. Dr. Grey’s specimen isin a hard, dark, mica-
ceous shale; and Mr. Carruthers, who has kindly examined this and the asso-
ciated fossil plants, says that it belongs to LZ. erenatum (Sternberg). On the-
same slab he observes portions of the stems of Calamites, perhaps of three
species, such as those that have a very slender periphery.—T. R.J.]
VOL. XXVII,—PART I, E
50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Deewie
laria*, Pecopterist, &c.; 7. Ferruginous sandstone, with a thick
dendrites weathered out on its surface, from the same place; 8.
Sandstone, with fucoid (?) markings, from the same place.
§ B. From the Carboniferous Rocks of Lower Albany.—1. Black
shale (slickensided), with Stigmaria; 2. Dark-grey granular quartz
rock, with pyrites, from near the shale.
§ C. Crystalline Rocks.—1. A variety of brownish steatite, fit
for carving, from the Transvaal; 2. Massive prehnite, from Bank-
berg, Cradock.
§ D. Crystalline Rocks from the Diamond-bearing Localities of
the Orange and Vaal Valley.—1. Block of calcite, from the Orange-
river district; 2. Specular iron-ore; 3. Galena; 4. Block of ecrys-
tallized quartz and galena; 5. Lydite, with pyrites; 6. Tremo-
lite; 7. Selenite; 8. Amethyst, quartz, agate, and garnet, from
the gravel.
Remarks.—With reference to A, No. 1, the direction of the pre-
valent currents of the Karoo formation might be learned from a
study of these rippled surfaces. No. 2. Excavating the shales to
examine if they would yield roofing-material, the author found these
little bivalves [which are Estherie, of a new species—T. R. J.].
They were found at one spot only. No. 3. These are water-worn,
and furnish evidence, the author thinks, of great aqueous denudation.
Their matrix is often, if not generally, permeated by igneous rock.
[These and other specimens have the appearance of bones imbedded
in volcanic ash.—TV. R. J. |
Of the country formed of the Karoo strata Dr. Grey observes :—
The sweet-grass country, Dutch ‘“ Zout-Veldt,” yielding the valu-
able Karoo plant (Adenachera parviflora) accompanies the Dicy-
nodon- (Karoo) beds of the great plateau, beginning on the eastern
side from about Queenstown, where the pasturage is of a mixed cha-
racter, locally “‘ Gebrokenveld.” From that district it is traceable
as in Bain’s map, with its margin and watershed on the Zuur-
berg &c. The author is inclined to think that the bones of the
Dicynodons were deposited in the shallow waters of an inland sea—
the salts of soda that predominate largely in the salines of the soils of
the great Karoo plains, and help to form the ‘‘back-grond” of
of that region (sandy soil impregnated with common salt and car-
bonate of soda +, and some salts of magnesia and alumina), sup-
porting him, he thinks, in this view §.
* [The cast of a portion of decorticated stem, in hard blue shale.—T. R. J.]
+ [In a dark shale. Mr. Carruthers regards this Pecopteris as being pro-
“bably P. Cistit (Brongniart). Alethopteris Lonchitidis, Sthg., and Asteroph yds
equisetiformis, Brg. also accompany the foregoing.—T. R. J.
t The ash of some native plant (‘“ Ganna- bush”) growing on the plains is
used extensively by the Boers in making hard soap, and contains a large per-
centage of carbonate of soda. The impure carbonate (lixivium), first mixed
with sheep’s tallow, is deprived of its carbonic acid by a long process of boiling,
requiring two or three weeks to be properly effected..
§ [The presence of Estheria, which, as a genus, inhabits brackish water, is in-
imical to the idea of an open sea having formed the Cradock beds, though in-
land brackish lakes would not be inconsistent. A fragment of an Encrinite (in
the Society’s Museum) in one of the brecciated limestones of the Rhenosterberg
1870. | GREY-—SOUTH-AFRICAN SPECIMENS. 51
No. 4. This was forwarded to the author by a friend, who found
it on his farm, at the southern margin of the Stormberg, a few
miles south of the outcrop of the coal there.
No. 5. This coal is from Mr. H. J. Baillie’s best coal at Andries’s
Nek. Dr. Grey states that some lignite occurs with it, and that
some of the coal near by is hard and anthracitic. The specimen was
taken not far from the surface ; and Dr. Grey observes that this coal
does not all burn very satisfactorily ; but some of it gives out a moderate
amount of heat, flaming for a limited time. Andries’s Nek is about
twenty-five miles north-east of Queenstown; and its coal is sup-
posed to be the same as that of the Stormberg.
The coal-seams show themselves mainly on the northern slopes
of the Stormberg range, where they are thin and shaly, alter-
nating with softish dark-coloured sandstones and purple marls.
They are from 400 to 800 feet above the base of the mountains,
and are exposed in the hills and ridges [of the flanks?]. The coal is
often pyritous ; and igneous dykes appear to have rendered much of
it anthracitic. Graphite, with black shales, has been found in
the north-western range of the Stormberg *.
Mr. Vice’s Stormberg coal, got by a shaft, sells at a fair rate at
the nearest villages. Considering the small population of the dis-
trict, the distance of the Stormberg inland, cost of transport, and
scarcity of labour, the Stormberg coal cannot be worked largely
as yet ft.
B, No. 1. {Mr. Carruthers remarks that, although this has some-
what the look of Cyclostigma, it is a true Sigillaria, with a root-
let, and that its stigmata are smaller and more numerous than in
any published forms.—T. R. J.]
The Lower-Albany coalfield is being explored by a Govern-
mental Survey. The reports are rather encouraging; but seams of
really good coal do not yet (summer of 1870) appear to have been
reached there. [In the micaceous shales of this series, collected by
Mr. Neate at Port Alfred, Mr. Bristow, F.R.S., has detected Szgzl-
laria, Stigmaria, Lepidostrobus, Halonia, and Selaginites, as re-
ported by him to the Colonial Secretary in May 1870.—T. R. J.]
D, No. 2. This in particular was sent to the author from a
spot where a large diamond was found. Dr. Grey visited the
diamond-yielding districts of the Orange and the Vaal some years
ago, and noticed the presence of primary crystalline rocks among
the gravel and in the tufa of the alluvium. He now remarks that
the conglomeratic alluvium is like that described as occurring in
Brazil and other places where diamonds are found. He doubts
the diamonds of the Vaal and Orange rivers having been derived
from the Draakensberg.
is almost, if not quite, the only marine fossil known in the Karoo beds (Quart.
Journ. Geol. Soc. vol. xxiii. p. 143).—T. R. J.]
* [See also Dr. Rubidge’s observations on these changes of the Karoo coal by
volcanic heat, Quart. Journ. Geol. Soc. vol. xii. p. 7.—T. R. J.]
+ [Notes by Mr. Evans and Dr. Atherstone on the Stormberg Coal were
published in the ‘Mining Journal’ of January 14, 1871.--T. R. J.]
E 2
52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 7,
To the Secretary of the Geological Society.
Yorktown, January 28, 1871.
Dear S1r,—Subsequent to the reading of Dr. Grey’s “ Notes on
some Fossils from South Africa,” it occurred to me that it is highly
probable that the upper or “Stormberg” division only of the
“Karoo formation” reaches so far north as the Orange-River Free
State, the middle and lower divisions never having been deposited in
that region. In this case, the Stormberg strata (of Secondary age)
containing the coal with Paleozamie (Atherstone and Stow) have
overlapped the Lower Karoo beds, and have been deposited directly
on paleozoic rocks continuous with those of the Transvaal. These old
rocks might well be of Carboniferous age, with old coal; for the
Devonian rocks appear to the north in the Transvaal ; and in Natal
the Karoo beds are said by Mr. Griesbach to occur in proximity to
the Carboniferous rocks, but unconformably and separated by igne-
ous intrusions. In the Stormberg, therefore, itis possible that the
Karoo coal-beds may be resting on the old Carboniferous rocks ; and
these latter may have yielded the really old coal-plants that have
been sent by Dr. Grey from the Stormberg section, and which were
also referred to by the late Dr. Rubidge some years ago.
Yours, &c.,
T. Rurrertr Jonzs.
2. On some points 7n SoutH-AFRican Grourogy.—Part II.
By G. W. Stow, Esq.
(Communicated by Prof. T. Rupert Jones, F'.G.S.)
[ Abstract*.]
THis paper commenced with a detailed account of the Forest zones,
coal, and other strata of the Karoo formation, as seen in sections in
-the Winterberg and Stormberg. The author particularly pointed
out the position of the Fern-beds at Dordrecht, of the Reptilian re-
mains found on the Upper Zwartkei, and of the Coal on the Klaas
Smits River. He next referred to the climatal changes of South
Africa, as indicated by its geology and fossils, particularly the
Karoo beds, the Hnon-conglomerate, the T’rigonia-beds, the several
post-Tertiary shell-beds, and especially the present surface conditions,
which he regarded as due to ice-action, as evidence of which he
adduces roches moutonnées, moraines, basins, and strie, both north
and south of the Stormberg, in British Kaffraria, and even in Lower
Albany. He concluded with remarks on the probable succession of
periods, and on the former existence of a great southern continent..
Discussion.
Prof. Ramsay expressed a hope that the author at some future
time would discuss the numerous subjects of which he treated at
* The publication of this paper is deferred.
1870. ] _ @RIESBACH—GEOLOGY OF NATAL, 53
greater length and under separate heads. He was not surprised at the
finding of plants of Carboniferous genera in the Dicynodon-beds which
appeared to be of Triassic age, inasmuch as the same was the case
to some extent in our own later beds of Oolitic date. He agreed in
the view of the probability of a vast continent having formerly ex-
isted in the southern part of the world, and considered that the
denudation of Southern Africa had been so great that it was no
wonder the boundaries of the old freshwater lakes were no longer
easy to find. It was also by no means surprising to him that a
recurrence of glacial phenomena should be found in Southern
Africa, as it had been in Europe. He did not, however, think it
necessary to call in the action of ice for the excavation of valleys
such as some of those described, as rain and running water appeared
to him sufficiently powerful for the purpose. At the same time
he would not deny the possibility of ice having been the agent in
these cases.
Mr. R. Tats had seen evidence of similar effects being produced
by aqueous force to those resulting from glacial action, and cited
instances of moraine-like deposits having been formed by running
streams in Central and Southern America.
_ Mr. H. Woopwarp suggested that it would be desirable to wait
for further particulars of the sections before assuming the actual
association of the Lepidodendron and other plants. He added that
the Stigmaria lately said to have been obtained from the Kim-
meridge Clay had really come originally from Newcastle.
_ Prof. T. Ruprert Jones remarked that Mr. Stow, like other South-
African geologists, had had ample experience of the effects of
violent rain. With regard to the mixture of Paleozoic plants (such
as the Lepidodendron &c. sent by Dr. Grey) with Paleozama and
Pecopteris, he thought it somewhat analogous to the mixture of
paleeozoic and mesozoic fossils in Australia.
3. On the Gzotocy of Nara, in Sours Arrica. By Cuaries Lupotr
GrresBacu, Esq., Corr. Member of the K. K. geologischen Reichs-
-anstalt, and of the K. K. geographischen Gesellschaft, Vienna.
(Communicated by Henry Woodward, Hsq., F.G.S.)
{Puates II. & IIT.]
I. GE0GRAPHY OF THE COUNTRY: WATERSHEDS.
Tue colony of Natal presents the appearance of a series of terraces ;
the first terrace begins to rise about thirteen to twenty miles from
the coast, and forms a hilly country, about 1000 feet above the level
of the sea. It forms plateaux in abrupt rising steps until it reaches
the height of about 2300 feet, after which the country sinks gradually
again to the level of Pietermaritzburg (2080 feet above the sea); but
54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. pDeck75
it soon rises again to the high plateaux of the Town Hill and Zwartkop
(about 5000 feet high). In a very few steps it forms the long and
mighty range of the Draakensberge, which form the great watershed
line between the rivers of the Atlantic and the Indian oceans. We
find in this range the Mont aux Sources (12000 feet above the level
of the sea), a knot of mountains, which sends spurs in five direetions,
forming the Witteberge and the Quathlamba Mountains. All these
great steps and plateaux run parallel to the coast, and consist of
more or less broad belts of country. The small belt on the sea-
shore shows tropical vegetation. The sugar-cane, the coffee, and
now recently the tea shrub, and the greatest variety of tropical fruits
find here suitable climate and ought to be sources of immense riches |
to the country if properly managed. When we ascend the first terrace,
the change in the landscape is at once remarkable, and the vegetation
has quite a different character. The sugar-cane and exotic ereepers
disappear, and their place is taken by more European plants; but
the coffee-shrub and many a fruit-tree strange to the eye of the
newly arrived European still remain. Ata still higher point these
remains of subtropical vegetation also disappear, and nothing is
visible to the eye but vast plains of “veldi,” stretching for miles,
covered with coarse-looking grass, and only interrupted by ant-hills
and deep holes made by the ant-bear (the worst foe of those most
industrious insects). Nothing more cheerful meets the eye in these
vast tracts than small hills and grass—grass everywhere—only
occasionally a lonely cattle-farm with the surrounding never missing
gum-trees, which give the place a still more lonely and cheerless
appearance. This belt is about thirty miles broad, and runs through
Kaffirland, Natal and the Zulu country. The succeeding, third district
is the most salubrious one, whose climate agrees best with the con-
stitution of Europeans. The soil is covered with a luxuriant grass
vegetation, which supports a strong and fine race of cattle. The
higher the ground ascends, the more fruitful it becomes; and on the
elevated plains, in the district where the yellowwood-tree flourishes,
wheat and almost all our European fruits will grow magnificently.
Here the winter, although not so severe as in northern Europe, is
more like the climate we are accustomed to, and is therefore a real
paradise to emigrants, who not only find a country where their
labours receive their best reward, but also a more genial climate
than the coast-district affords. Natal’s rivers flow to the Indian
ocean and supply the colony with abundance of water, which makes
its soil superior to that of the “old eolony,” with its vast plains,
“‘karoos,” and dreary ‘“ veldts.”
II, Guonoey.
The geological structure of the country is shown by the map and
section on Plate II., in the preparation of which the author has sup-
plemented the results of his own researches by those of Dr. Suther-
land and M. Franz Groéger.
1. Granite and Gneiss—Granite in South Africa does not form
the centre of the country or the most prominent of the elevations.
1870. ] GRIESBACH—GEOLOGY OF NATAL. 35)
It is only visible at the lowest parts of the river-valleys and near
the coast, in fact wherever the river, by its erosive action, has re-
moved the sedimentary rocks. If we draw a straight line from the
Umtwalumé river due north, we shall touch all those parts of the
country where granite and gneiss reach the surface through the
covering of stratified rocks. Granite, as Livingstone correctly ob-
serves, forms the bones of the country, which at places are seen
through theskin. It only forms hills and the bottoms of river-valleys.
The granite is mostly a fine-grained grey variety; sometimes it
becomes very coarse and contains large crystals of feldspar ; alto-
gether it has the same appearance as the granite at the Cape, which
Hochstetter first described as similar to the Karlsbad granite. At
some places there is a red variety, in which the quartz and mica nearly
disappear, being a mere feldspathic rock, in which decomposition
reaches a great depth, when it presents a kaolin-like appearance,
similar to that found by me at the Umzinto and at the Jfafa river.
Further to the south, at the Umtwalumé, Ehlongeni, and Umkobe
rivers in Alfredia, the belt of granite becomes broader, and repre-
sents a distinct zone. The greatest elevation is reached by the granite
in the counties of Victoria and Umvoti, where the Noodsberg group of
mountains and all the surrounding country, and the bottoms of the
valleys of the rivers Umvoti and Tugela, in the latter very far
up, consist principally of this rock. I have found gneiss at several
places, as, for instance at the base of the Sluten-Konga (Mount of
Mist), at the head-waters of the Umtwalumé, &c.; but nowhere
was it practicable to map it, as the high grass vegetation rendered
surveying quite impossible. The granite is traversed in all directions
by quartz-veins, which seldom have a thickness of more than from
about 1 inch to 2 feet. The quartz itselfis a beautiful white variety,
almost like glass, which, besides occurring in veins, is very frequently
met with in large masses, called “ reefs,” which usually very soon thin
out towards their base. These quartz masses were always a subject
of great interest in Natal, as it was thought that they would yield
gold in paying quantities. Such is actually the case at almost all
places, but not in sufficient quantities to yield a profit for crushing
it. At the Umzinto-river valley, after a long time occupied in
searching, I succeeded in finding small traces of gold in a variety
of grey granite, which also reminds one much of the granitite of
Bohemia. The alluvium there also contained gold, but only in traces,
and not nearly sufficient to pay any one to work at it.
2. Mica-schists, Clay-, Chlorite-, and Talcose Slate formations —AlL
these slate formations are to be met with at places where the gra-
nite base is laid bare; and everywhere the slates stand nearly up-
right, at an angle of 70-75°, with a strike from north to south.
The clay- and talcose slates are very well seen at the Umzimculuana
(little Umzimculu), in the county of Alfred, and at the Tugela, at
the junction of this with the Umziniaty river, and also at the Ite-
mani, a small tributary of the Tugela. At the Umpampinioni river
a dark grey clay-slate, dipping at an angle of about 40° and striking
from south to north, possesses considerable thickness (about 200
feet or more). It rests on granite, and underlies and is conformable
56 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 7,
to the overlying sandstone, to which it belongs, as I think, and not
to the older clay-slate formation. It is remarkable that at the
Tatin (so-called ‘‘ goldfields ”’”) the slate formations have the same
strike and are elevated at the same angle of about 70°. At the
mouth of the Umzimculu, about seven or eight miles from it, and
north of the young township of Murchison, the river breaks through
crystalline limestone of enormous thickness, but whose position
relative to the neighbouring strata is not clear. On both sides
of the valley the limestone forms precipitous walls of some 1000—
2000 feet, which are luxuriantly covered with vegetation. Also the
bottom of the river consists there of the same rock, the thickness
of which towards the base is not known. On the surface it only
covers a space of about four square miles.
3. Table-Mountain Sandstone.—The sandstone plateaux, which
are so characteristic of the African landscape, lie perfectly hori-
zontally upon the old slate formation, and at some places upon the
granitic base. The sandstone, forming precipitous tableland, has
never been disturbed; nowhere is a folding of the deposits visible ;
only fractures run through the zone, in which masses of Aphanitic
Diorite are seen, which have burst through the granite and slate
formation ; but nowhere is the sandstone raised up at an angle, or
folded by the greenstone. The high plateaux are covered with a
dense grass vegetation ; and numerous herds of cattle feed on the
level summits of the tableland. The soil is extremely poor, and
there is not even a shrub to interrupt the endless uniformity of
the landscape. The rivers have made their way through the beds
and strata of this sandstone, thus forming precipices, at some points
‘several thousand feet in height. The sandstone shows the same litho-
logical peculiarities as the 'Table-Mountain Sandstone of the Cape,
after which it is named. The tops of many of the “ table moun-
tains ” of the Colony are crowned by beds of a dark basaltic green-
stone (fig. 1) which also possesses the same pillar-like structure as our
basalt. It contains fragments of quartz, granite, and gneiss. Ina
variety of this igneous rock, from the ‘‘ Great Karoo,” I found small
traces of gold. I never found any organic remains in the sandstone
of the Colony itself, except in a thin soft shale, with much mica in it,
which seems at the Krantzkop (fig. 1) to be a bed in the sandstone,
from which I got some small bivalves and a finely striated Patella,
both too indistinct for determination. Such shale is also exposed
near the upper drift of the Umkomaz river, near Richmond, and at
several other places in the Colony. The Sluten-Konga, Table Moun-
tain near Pietermaritzburg, Inanda, and Noodsberg are examples
of the regular-shaped table mountains of South Africa. The same
shales and quartz-sandstone form the Krantzkop, which drops nearly
vertically down to the Tugela river, about 3800 feet. The high pla-
teau of it is eapped with melaphyre-like greenstone. The basis of
the Tugela valley is granite, intersected by dykes of an aphanitie
diorite. The slate formation, the layers of which stand almost
vertical, rests on the granite and is covered with the so-called
“‘ Doorns,” the celebrated mimosa vegetation of South Africa: the
great mass of the mountain is built up of sandstone, and crowned
1870.] GRIESBACH—GEOLOGY OF NATAL. 57
with basaltic greenstone. In this locality, but on the Itemani side
of the Krantzkop, I found the small traces of organic remains in the
shaly bed of the sandstone which I mentioned above.
Fig. 1.—Section through the Krantzkop Mountain.
: Valley of the Zulu
Itemani River. Krantzkop, 3800 feet. Tugela River. Country.
=>—
7 All,
Myo ly
ee Y TELE
1. Granite. 2. Aphanitic diorite. 3. Mica- and talcose slates. 4. Table-
Mountain Sandstone, with, 5, thin layers. of a sot shale containing a few
traces of fossils. 6. Melaphyre.
4, The Karoo Formation.—So called after the Karoos, the im-
mense plains of the interior, as they are principally composed of
strata of this formation, which has its greatest height above the sea
in the Draakensberg range (see Section, Pl.II.). The lower part of
the land on the Natal side of this range rests partly upon the Table-
Mountain Sandstone, but not conformably. The Karoo sandstones
and shales occupy the largest portion of South Africa, as they com-
pose the whole of the interior, forming the high elevated plains of
the Kalahari, the Free States and the Transvaal, as well as the coun-
tries to the north as far up as the Limpopo; they are also to be met
with at the Zambezi. As Mr. Tate, and Profs. T. R. Jones, Owen,
and Huxley have already so ably described this formation with its
fossil contents, little remains for me tosay. The dark-grey and blue
shales of Pietermaritzburg, containing oxide of iron in great quan-
tities, represent the Hcca-beds of the great Karoo. Further up it
passes gradually into sandstones of much the same lithological cha-
racter as the Table-Mountain Sandstone, with intervening layers of
shale, which at Ladysmith, Newcastle, in the Tugela valley, We.
contain beds of coal. Numerous remains of reptiles and plants are
described, which come from the Natal side of the Draakensberg; and
therefore the age of these beds may be determined. Mr. Tate regards
them as Triassic, whilst Mr. Wyley thinks that they belong to the Car-
boniferous period; but as the coal from Tulbagh, in the Cape Colony,
is decidedly carboniferous (Calamites, Equisetum, and Lepidodendron
in the sandstone), and the succeeding Karoo formation (which is a
freshwater deposit) does not lie conformably on the former, Mr. Tate’s
opinion seems the most acceptable. Also the same formation, with
Dicynodon and Glossopteris Browniana, occurring in India at the base
of the cretaceous series, is proved, by a careful examination of its
flora, to be a Triassic deposit. There can certainly not be the
slightest doubt that the Natal coal belongs to a far younger period
08 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 7,
than the Tulbagh coal, which is an equivalent of our Coal-mea-
sures.
The “ Karoo formation ’”’ also occurs in a small belt on the sea-
coast of Natal, which belt is never broader than from seven to eight
miles, if so much. Beds of the Karoo series are well exposed at
the Umgeni mouth and also at the Ifumi river. Any one who has
been to Pietermaritzburg must have observed cuttings on the
road, about seven or eight miles before he reaches the capital, in a
dark shaly rock, with large boulders of older rocks imbedded, of
granite, gneiss, slate, and also frequently of greenstone (fig. 2).
These boulders are so characteristic of African scenery that they
have received general attention. The boulders, often of very large
size, are imbedded in a soft grit and shaly clay, containing small par-
ticles of mica.
Fig. 2.—Irregular boulders of Greenstone, sometimes Granite or
Gnerss, imbedded in clay and grit.
we
ome
YAN
The boulders seem to have been formed on the spot, or at least
have not travelled very far, as many of them have kept their angular
shape, and they seem to have undergone rather a process of decom-
position than of rolling. These beds (“ boulder-beds”) extend often
over a very large area, and pass everywhere beneath the dark shale,
which represents the base of the Karoo plant-beds. This is proved
by a section at Thornville, and also on the sea-coast of Natal at
several places, amongst them at the Umgeni valley and the Ifumi
river. At the Umgeni and Durban the sections are as in figs.3 & 4.
Both these sections show that the plant-bearing shales and sand-
stones rest unconformably on the older Table-Mountain Sandstone,
and also that the boulder-bed lies at the base of these plant-
beds.
The same is shown at part of the road between Pietermaritzburg
and Thornville (see Section, Pl. IT.).
The boulder-bed here, in the same way as in the other sections,
passes gradually into the shale of Pietermaritzburg, which, as I
think, belongs to the lowest bed of the Karoo series. We learn from
the Geological Survey of India that almost the same formation of
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60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 7,
shales, sandstones, and calcareous grit contains the same forms of
plants, as well as reptilian remains of Dicynodon, and lies conform-
ably on a boulder-bed, which gives the impression that it was formed
on the spot, and was not transported by the action of water. It
is also remarkable, and an observed fact, that this boulder-bed of
Southern India passes gradually into the succeeding shales and
sandstones, which have been termed by the Indian geologists “the
Ootatoor plant-beds.” <A lithologically similar boulder-formation I
have also seen at the same horizon in the Cape Colony, passing
beneath the blue Karoo shales; and I am pretty certain that Mr.
Bain and many of our African geologists have taken this boulder-
bed, at many localities, for an igneous trappean rock. Mr. Bain (see
his map) calls this boulder-bed, which dips under the “ Kcca-beds ”
of the ‘‘ Pataties Revier,” ‘ Claystone Porphyry.” There is certainly
a basaltic melaphyre, forming beds of considerable extent in this
lowest part of the Karoo formation, as, for instance, can be seen
near Platte-fontein, in the great Karoo; but this trap does not
belong to the extensive beds of boulders at the base of the “ Pata-
ties Revier” shale. At first sight the trap and the boulder-bed
have many similarities, as the material of the boulders is partly de-
rived from igneous rocks. Dr. Sutherland thinks that the boulder-
bed was formed by glacial action, and tries to prove it by the ob-
served fact of grooves and furrows on the plateaux of the Table-
Mountain Sandstone. These grooves, quite similar to those in our
Alps, occur in great abundance on the sandstone of the Ifumi river,
about twenty miles south of Durban.
The greenstone (melaphyre ?) has found its way through this for-.
mation at many places, and forms beds between the strata of it.
The greenstone contains a great quantity of pebbles of older rocks
imbedded, which give it a speckled appearance. But it seems that
the greenstone eruption happened at the earliest period of the form-
ing of the Karoo beds, as the “‘ kopjes” of greenstone are only found
in the lowest strata of the “‘ Pietermaritzburg shales,” and in the suc-
ceeding sandstones. The series of greenstone ‘‘ kopjes,” which runs
from the Ingeli Range in Kaffirland up through Richmond, York,
and Greytown to the Tugela river, is of practical importance, as in
it, or in the direction of its strike, the occurrence of copper ores can be.
traced through the whole of South Africa. Besides this Trappean
greenstone, a second igneous formation may be found within the
Karoo series, the so-called amygdaloid rock, which caps many of the
heights of the upper Karoo beds, and often forms extensive beds be-
tween them. From it are derived the various kinds of chalcedony,
agates, rock-crystals, and topazes which are so plentiful in the
rivers of the Free States and Natal.
5. The Cretaceous Rocks of South Africa.—Between the rivers
Umtamfuna and Umzambane, about five miles from the southern
boundary-line of Natal, on the south-eastern coast of Africa, some
deposits are found which at first sight seem to be of the same ma-
.1870.] GRIESBACH—GEOLOGY OF NATAL. 61
terial as the underlying stratum. They consist of sandy marls and
hard sandstones of a greyish-brown colour, with a few calcareous
concretions. These rocks are partly covered at high water by the sea,
which has hollowed out small cavities in them (Fig. 5). They have
probably served at some period as a shelter for white people, as the
natives of this district call them “ Izinhluzabalungu,” houses of the
white men. These rocks only extend for a short distance, and only
form isolated cliffs. They are found, too, at the Impengati river, and
at some of the more southern rivulets which run into the sea be-
tween the boundary of Natal and the St. John’s river(Umzimyooboo).
The same are also recognized in the bed of a small stream, running
into the St. Lucia bay, in the Zulu country. The strata forming hese
deposits are perfectly horizontal, and they rest upon a sandstone of
much older age, which belongs to the very interesting series of the
Karoo formation. It is remarkable that the Tzinhluzabalungu
rocks do not rest conformably upon the older formation, the plant-
bearing sandstones.
Fig. 5.—Izinhluzabalungu Caves.
a, Karoo shales and sandstones. 6. Sandstone with fossil wood &c. c. Tri-
gonia-bed. d. Ammonite-bed. ¢. Gasteropoda-bed. f. Zone of Ame
monites Gardent.
I have been enabled to distinguish no fewer than five distinct
faunas. The lowest stratum is a hard calcareous sandstone (6), very
much worn by the sea breaking against it at high water. Large
trees and branches are imbedded in it, lying about in all directions,
The wood is traversed by large masses of Z'eredo, whose holes are
filled with iron pyrites. Resting on this stratum is a bed of softer
brown sandstone (¢), with great abundance of Trigoniew. This bed is
more exposed near the Umzambane river, and nearly concealed at
the northern end of the deposits. It is overlain by sandstones and
grits (d), containing Ammonites, resting upon which is a softer
sandstone and grit (e), containing many fossils, mostly bivalves and
Gasteropods. The roof of the caves is formed by a harder lime-
stone stratum (f), which has not been so easily worn away by the
sea as the underlying sandstone stratum. This limestone contains
Ammonites Garden, Baily.
62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 7,
Fauna of the Izinhluzabalungu deposits.
Equivalent
Species. Stratum. in Northern
Europe.
Ammonites Gardeni, Bavly............ Harder brown
Fossil bones, wood, &c. ............... limestone (/).
White chalk
most probably.
——_—
Pugnellus uncatus, Morb.............4.. )
Fasciolaria assimilis, Stol. ............
Fasciolaria rigida, Baily ............4..
Tritonidea trichinopolitensis, Ford.
Scalaria turbinata, Ford. ...............
Solarium Wiebeli, nov. sp. ...........-
Chemnitzia undosa, Ford. ............
EKuchrysalis gigantea, S¢ol. ............
Solariella radiatula, orb. ............
Avellana ampla, Stol. ...........:0060+-
Natica multistriata, Baily ............
Pollia pondicherriensis, ford. .........
Lagena nodulosa, Stol..............4.++.
Cerithium (Fibula ?) detectum, Sol.
Cerithium kaffrarium, nov. sp. ......
Turritella multistriata, Mss. ......... stone and grit,
IDeioteAIUOIN, FEE cenoreonencacssoedsancos aiid, imeem
Ostrea; ispeei fl Saye oy UE eee Ne. | fossils (e). |
a
Soft brown sand- Probably
Upper Green-
sand,
Cretaceous period.
Pecten quinquecostatus, Sow. .........
Pecten amapondensis, n. sp. ......... |
ANIED) CHOSE, IMs Si Sbsancnecarnodadccse ace
Arca natalensis, Baily ...........-0se-
Pectunculus africanus, n. sp. .........
Trigonia elegans, Batly...............+.. |
Cardium denticulatum, Bazly .........
Cardium Hillanum .....................
Venus arcotensis, Ford...................
ASEATLO,YSPsce sen cjencatsacue sce sees -eaetee
Inoceramus expansus, Baily .........
Hemiaster Forbesii, Badly ............
Holaster indicus, Ford. ...............
Miademayspecwenscecene eee
Ammonites umbolazi, Baily ......... )
Ammonites Soutoni, Baily ............
Ammonites Stangeri, Bazly............ Sandstone and | Bigeee
|
|
y
Ammonites rembda, Ford. ......... grit, very much Gueonend
Ammonites Kayei, Mord. ............... like the above (d).
Anisoceras rugatum, Ford. ............
Trigonia Shepstonei, nov. sp. ............ Hard sandstone(c).
———
Fossil wood, with Teredo............... very much water-
worn (0).
Hard sandstone,
¢ Karoo sandstone oes
Faint plant-remaing .,................... a Ey shale g(a). fo ... Triassic ?
1870. ] G@RIESBACH— GEOLOGY OF NATAL. 63
Description of Species.
Genus AMMONITES.
There are four species described in Mr. Baily’s paper, to which I
have to add two more, both of which are fom in the Cretaceous
series in Southern Taf:
One of the commonest species in this formation is
AMMONITES UMBOLAZI, Baily. Pl. III. fig. 1.
A fine and characteristic form, which is not quite distinctly
figured in Mr. Baily’s paper. The flexuous ribs on the well-preserved
shell are not so strongly marked as in the figure, and do not show the
least tendency to form tubercles near the back, but gradually die
away in all the specimens I have seen. Number of specimens 26.
Locality. Umtamfuna river, South Africa, from bed d.
AMMONITES REMBDA, Forbes. PI. ILI. figs. 2,3
The whorls are higher than wide; it possesses a remarkably
shaped keel. The shell is well preserved. It has distinct furrows,
which are about 6 to the whorl, and are slightly bent near the keel,
towards the mouth. The suture is easily detected; 6 lobes and 6
saddles can be made out. The dorsal saddle is tripartite, the next two
lateral saddles bipartite, and the next three only single saddles. The
dorsal saddle is double the height of the dorsal lobe; the lateral lobes
are very deep; the lateral saddle is of the same height as the dorsal
one; but the succeeding ones decrease very rapidly in size. Forbes’s
figure of this Ammonite is very indistinct; so also is the fragment
which is figured in the ‘ Memoirs of the Geological Survey of India.’
Ammonites rembda, from Pondicherry, is in every particular like
our African specimen. The shell is perfectly smooth, and shows in
some places beautiful colours. There are some small specimens
amongst the collection, which seem to me to be only young indi-
viduals of A. rembda. Number of specimens 3.
Locality. Cliffs on the sea-shore, between the rivers Umtamfuna
and Umzambane, in Kaffirland, from bed d. Pondicherry, in India.
Age. Probably Cenomanian. India, Valudayur group.
Ammonites Kayet, Forbes.
An excellent specimen, with flexuous ribs, and a few furrows
parallel to the ribs. The ribs are very fine and narrow, and ge-
nerally divided into two or three at about the middle of the whorls.
There cannot be the slightest doubt about the identity of the African .
specimen with Ammonites Kayet, as it shows all the remarkable pecu-
liarities of Forbes’s original specimen in the Collection of the Society.
Locality. Umtamfuna river, from bed d. Pondicherry, west of
Penangoor, and north of Odium, in the Trichinopoly district.
Range. Cenomanian. In India, the Valudayur and Ootatoor groups.
ANISOCERAS RUGATUM, Forbes. PI. III. fig. 4.
My specimen shows sharper ribs than the Indian form; and as
it is only a fragment, it does not allow a very distinct specification.
Locality. Umtamfuna river. Bed d.
In India. The Valudayur group.
64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 7,
Remarks. Altogether there are 15 species of Cephalopods described
out of this bed, three of which are also found in the Valudayur
group of Southern India. Only two species belong to a higher
horizon, one of which occurs in India in the Arrialoor group.
Name. ° In India. ; Relationship. Range.
Ammonites Soutoni, Baily. . Ootatoor ? A. implatus. |Ootatoor group.
—— Stangeri, Badly.
—— Gardeni, Baily......... Arrialoor A. Gardeni. |Arrialoor group.
—— umbolazi, Bazly.
rembda, Forbes ...... Pondicherry. A.rembda. | Valudayur gr.
—— Kayei, Forbes ......... Pondicherry and | A. Kayei. | Valudayur and
Trichinopoly distr. Ootatoor group.
Anisoceras rugatum, Forbes; Pondicherry. | A. rugatum. | Valudayur gr.
There is only one quite strange form ; all the others are found or
have their representatives in the Indian Cretaceous series. We see
that four out of seven species belong to the lowest beds of the Indian
Cretaceous formation, to the Ootatoor group and the Valudayur
group, and only one, A. Gardeni, belongs to a higher horizon, the
Arrialoor group, which resembles our white chalk.
Crritaium (Fisvia ?) pETEcTUM, Stol.
Pal. Ind. fig. 192, pl. xv. vol. i.-iv.
This species is found in the same deposits. Shell perfectly smooth,
with scarcely visible lines of growth, and very thick.
Locality. Umtamfuna. Bed e.
CERITHIUM KAFFRARIUM, noy. sp. Pl. III. fig. 5.
Spiral angle 40°. Number of whorls 9.
_ The shell is very characteristically ornamented—coarse and trans-
verse ribs, which are intersected by thin spiral lines. Each of the
whorls is contracted near the suture, forming a deep furrow.
Locality. Umtamfuna river, from bed e:
TURRITELLA MULTISTRIATA, Rss.
Sowerbi, Forbes.
Bonet, Baily.
Mr. Baily, in his paper, looks upon this Turritella as a new species ;
but it agrees perfectly with Mr. Forbes’s original in the Collection °
of the Geological Society ; his figure is not very clear, which may
account for the making of a new species, as the African specimen
has nothing in its characteristics which could enable any one to di-
stinguish it from the Indian species. :
Locality. Umtamfuna river, bed ¢. Pondicherry, Trichinopoly
group.
ScALARIA TURBINATA, Forbes. Transact. Geol. Soc. vil. p. 127,
pl. xii. fig. 18.
Scalaria ornata, Baily.
Mr. Baily’s specimen not only agrees with the Indian Scalaria in
the description and figure, but more so even upon a careful examina-
1870. ] G@RIESBACH—GEOLOGY OF NATAL. 65
tion of the well-preserved original ; it seems, therefore, to me not rea-
sonable to create a new species because it is derived from a different
locality, but shows again the coincidence of the African and Indian
Cretaceous deposits.
Locality. Umtamfuna river, bed ¢. In India: Pondicherry.
Sorartum WIsBELI, nov. sp. PI. IIT. fig. 6.
Angle 130°. Number of whorls 5.
The surface perfectly smooth, only the lines of growth are faintly
visible ; but neither transverse striz nor ribs can be distinguished,
as in Solarium pulchellum, Baily, from the same stratum ; in shape
also this species varies much from Baily’s Solarium, which pos-
sesses gradually widening whorls, whilst in the present species each
whorl is double the width of the preceding one.
Locality. Umtamfuna river, bed e.
CHEMNITZIA UNDOSA, Sow., spec.
Chemnitzia undosa, Forb.
Scalaria undata, D’Orb. __
Turritella (Chemnitzia) Meadii, Baily.
Chemnitzia Sutherlandit, Baily.
Mr. Baily calls a small Chemnitzia, which shows slight spiral lines,
Turritella Meadii; but it is, I think, only a young individual of
his new species Chemnitzia Sutherland, which can be identified
with some varieties of Chemnitzia undosa, Forbes. The last whorls
do not show the transverse lines so distinctly; and altogether it is
impossible to find two specimens which show exactly the same
ornamentation of surface. The older whorls are always more di-
stinctly ribbed, but not the later ones. In full-grown specimens,
the spiral lines, which even in young ones are very feeble, dis-
appear. |
Locality. Umtamfuna river, bed e. In India: Garudamun-
galum, Kulligoody, Alundanapooram, Serdamungalum, Anapaudy,
Andeor. ‘Trichinopoly group.
EvucurysaLis GIGANTEA, Stol.
This is the species erroneously referred by Bailey to Turritella
Renauxiana, D’Orb.
Locality. Umtamfuna river, bed e. In India: north of Alun-
danapooram, east of Anapaudy, Comarapolliam. Trich. & Arr. Gr.
DENTALIUM, spec.
A small fragment of a smooth Dentalium, which it is not possible
to identify with any already described species.
BIVALVES.
Fam. I. OstreipZ.
OstREA, L., spec.
Numerous small specimens, imbedded in the sandstone with Am-
monites and other shells, beds d and e.
VOL. XXVII.—PART I. F
66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 7,
PECTEN QUINQUECOSTATUS, Sow.
Very numerous in this locality, resembling in every respect the
specimen from Pondicherry in Mr. Forbes’s Collection in the Geo-
logical Society’s Museum.
Number of specimens obtained by me, 11.
Locality. Umtamfuna river, bed e.
PECTEN AMAPONDENSIS, noy. sp. PI. III. fig. 7.
The right valve very slightly concave, finely striated concen-
trically, with broader radial ribs. Towards the end of the valve,
two distinct concentric lines, which divide the surface of the valve
into two or three areas.
Locality. Umtamfuna river, bed e.
ARCADE.
ARCA CAPENSIS, nov. sp. Pl. III. fig. 10.
The valves very thick, surface nearly smooth, very slightly can-
cellated, margins smooth. Huinge-teeth numerous, the lateral ones
very strong. The ligamental area with numerous but very narrow
grooves ; for the cartilage is much smaller than in Arca natalensis,
and the interior umbones nearly touch each other in closed valves.
Arca trichinopolitensis, Forbes, is very nearly allied to this species.
Mr. Baily’s figure of Arca umzambaniensis does not suffice to enable
me to decide positively whether the present species is distinct from
it; but it seems to me that Mr. Baily’s figure represents a much
flatter specimen than mine.
Number of specimens 9.
Locality. Umtamfuna river, bed e.
PECTUNCULUS AFRICANUS, nov. sp. Pl. III. fig. 8.
A small bivalve ; length about from 3—? of an inch. Surface finely
radiately striated, showing lines of growth ; margins denticulated ;
hinge semicircular, teeth transverse ; ligamental area very small.
This species is most nearly related to P. subawricwlatus from Pondi-
cherry (see Mr. Kaye’s Collection) ; but the latter is more circular in
form than P. africanus.
Number of specimens collected, 41.
Locality. Umtamfuna river, bed e.
TRIGONIAD ZZ.
TRIGONIA SHEPSTONEI, nov. spec. Pl. III. fig. 11.
This species stands between T’rigonia crenulata and scabra, Lamk.
The surface shows strong lines of growth, with thick transverse ribs,
which run quite straight from the beak to the margin, and form
right angles with the ventral margin. The ribs have very pro-
1870. | GRIESBACH—GEOLOGY OF NATAL. 67
minent tubercles, which become stronger near the ventral margin.
The teeth are 23, the left divided and striated. The surface is
divided near the posterior margin longitudinally by two or three
furrows into as many areas, transversely striated and ribbed. The
ribs are slightly curved, and in the inner carina they stand perpen-
dicularly to the posterior margins. 7. Shepstone: shows distinct
differences from Trigonea elegans, Baily, in its strong and thick
tubercles, in the general rough surface of the valves, and also in
its shape. Our species is thicker, and the ventral margin is plicated.
Very common, forming entire beds in the sandstone. This species
seems to have been commoner at the base of the stratum ; but the bed
is not divisible into different horizons.
Named after the Hon. Theophilus Shepstone, the Secretary of
Native Affairs tn the Colony of Natal.
Locality. Umtamfuna river.
CARDIADA.
CARDIUM DENTICULATUM, Baily. Pl. III. fig. 12.
To Mr. Baily’s description I have only to add that the pallial
line is simple, and not in the least sinuous. Cardinal teeth 2;
lateral ones 1, 1.
A small Astarte seems to be not uncommon. A Teredina is also
found in large masses in fossil wood at the lowest part of the deposit.
EcHINODERMATA.
Hemraster Forsusit, Baily.
Honaster rnpicus, Forb.
Drapema, sp. Pl. III. fig. 13.
Table of the Range of the Fossils of the Umtamfuna River.
Cephalopoda.| Gasteropoda. | Bivalves. | Hchinod.
Vow ee
|
7
New species, or peculiar to ; ( 3 of these |
the African locality ...... 1 | 4 4 {nearly al- [ 1
; lied to
i | Ind. sp. | )
In.the Arrialoor group ... 1 3 P04 2
Trichinopoly group......... 2 11
| Ootatoor and Valudayur
ly aberoups,- Lidia ../..caae. 4 1 or 2) Nu
| ‘Total of species which also
occur in India ............ 5
ret
—
oo
e
bo
bo
F2
68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 7,
Gasteropoda of the Umtamfuna River which also oceur in India.
Localities in India, where
Name. i
the species also occur.
Pugnellus uncatus, ford. ...... Parchairry, Kulligoody...... Trichinopoly gr.
Fasciolaria rigida, Bazly...... Andoor, Coonum, Shutanure/Trich. group.
Fasciolaria assimilis, Stol. ....\Olapaudy ..............2.-+266 Trich. gr.
Tritonidea trichinopolitensis|Anapaudy ..................--- Trich. er.
Pollia pondicherriensis, Forb.|Alundanapooram ............ Trich. gr.
Lagena nodulosa, Stol.......... OlapaudyPyecieee ens svane- eee Arrialoor gr.
Cerithium (Fibula) detectum,
SCOEs Ure Coe wa Aenea cena Kear pad iyjienssdatarseseey -eree Arrialoor gr.
Turritella multistriata, fss.../Pondicherry .................. Trich. gr.
Scalaria turbinata, Ford. ...... IRondichenny i asaccceey sank Trich. gr.
Chemnitzia undosa, orb. ...|Pondicherry .................. Trich. gr.
Huchrysalis gigantea, Séo/. ...|Alundanapooram, Comara-
polliamiieeesesseeceeeeeeeees Trich. & Arr. gr.
Vylapaudy, Olapaudy,
Comarapolliam, Arri- es
: ‘ DOOD EE acaen secs see aceon rrialoor gr.
Solariella radiatula, Ford. ... Andoor, Kalakonuttom....|Trich. gr.
Puravoy, Moraviatoor,
@diumy gee eee Ootatoor gr.
Avellana ampla, Séo/. ......... N.W. of Veraghoor ......... Trich. gr.
It is quite clear that most of the species obtained from this African
locality (‘‘ Izinhluzabalungu”’) resemble in every respect those of
the Trichinopoly series of India. The Trigonia beds with Ammo-
nites Kayer, A. Rembda, &c., show the true character of the Ootatoor
beds of the Trichinopoly district, whilst we have the Trichinopoly
group represented by eighteen species, which also occur in India.
The Arrialoor group is proved only by Ammonites Gardeni, which
-was first described from Africa, but has since been found by Stoliczka
in the Indian Cretaceous series.
The plant-beds with Teredo find their representative in the lower
beds of the Ootatoor group of the Trichinopoly district; and from this,
and also the fact that the preceding plant-bearing Karoo formation
finds its analogue in the Indian Ootatoor plant-beds (not the Oota-
toor group), the conclusion is easy to arrive at, that both Africa and
India were, after the development of the Table-Mountain Sandstone,
one continuous continent, which afterwards was covered by the
Cretaceous sea.
Between the deposition of the Table-Mountain Sandstone and that
of the plant-bearing blue shales and of their Boulder-bed, which
form the base of the extensive Dicynodon-sandstones, a long time
must have elapsed.
The large area, now covered by the Indian Ocean, must have been
the basin for an extensive series of lakes, which would explain the
occurrence of the same plants and large reptiles which were then
living in India and also in South Africa. It must have been a
period of long-enduring tranquillity, and no great disturbance what-
ever seems to have occurred. These periods of repose, which wit-
1870. | GRIESBACH——GEOLOGY OF NATAL, 69
nessed so very few changes during the deposition of at least 5000
feet thickness of strata, must have lasted through the Triassic age
right up to the Upper Jurassic; as in India the highest of these
beds seem to belong to the Jurassic formation. The greater portion
of the Indian Ocean must, at this period, have been depressed, to-
gether with a large part of India and Southern Africa, which were
covered with the shallow Cretaceous sea, having a peculiar fauna of its
own. ‘The Cretaceous deposits of Southern India and Africa were all
shallow-water and coast-deposits, as is proved by the species of fossils
they contain and also by the quantities of wood imbedded in them, which
give evidence of a formation on a shallow coast, where the wood was
soon covered with sand and mud and in this way preserved. Since
that period the coast has been gradually rising, or the sea retiring. The
portions of the Cretaceous sea nearest the old coast-line had become
dry land; and we see the remains of these deposits in Southern India
and Africa. There cannot be the slightest doubt that the upheaval
of the country is still going on; for along the whole coast of South
Africa, from the Cape to Durban Bluff, and still further north,
even as far as Zanzibar, modern raised beaches *, coral-reefs, and
oyster-banks may everywhere be seen. At the Izinhluzabalungu
Caves is such a point, where the rising of the coast is plainly visible ;
recent oyster-banks are now 12 feet and more above high-water
mark. The same can be observed on the whole line of the Natat
coast. Vander Decken has observed the same thing at Zanzibar,
and is of the same opinion as myself, viz. that the eastern coast is
rising. arly in the present year I had the opportunity of observing
at the Bazaruto Islands, about 90 miles to the north of Inhambane,
on the east coast of Africa, a series of raised coral-reefs round the
island of Marsha, containing many living shells and quite recent
oyster-banks. In fact, I believe that the Bazaruto Islands only owe
their existence to the circumstance that the coral-reefs have been
upheaved, and that their surface was naturally covered with loose
sea-sand, which is the only soil of these desolate islands. Every-
where, at about 12-14 feet depth, water is to be obtained at Marsha ;
wherever the sand is removed the coral-rock is reached.
What with this constant rising of the land and the consequent
shallowing of the river, I do not believe that the Port of Durban
has much hope for the future, as some day the entrance to the
harbour, which is not very deep at present, must be blocked by a
bar across it like most of the African ports. The only exception to
this rule is the large Port of Delagoa Bay; the port is cleared of
sand and mud by nature itself. It was evidently formed by the
north and south current of Mozambique, which has gradually hol-
lowed out this fine bay. Between Elephant Island and the terra
jirma the current enters the bay, and, turning round in it, returns to
the sea between Elephant and Inyack Islands, in this way always
keeping the entrance open by its scouring-out action.
* The writer has seen implements of early man which were obtained by
Richard Thornton and others in old raised beaches at Natal, near Inanda, and.
at the mouth of the Zambesi River.
70 PROCEEDINGS UF THE GEOLOGICAL SOCIETY. Weer
If we take a vertical section of the Natal formations, we shall find
them as follows :—
Brown soft sandstones and grit, with great | Cretaceous Series, Lower Greensand
numbers of fossils. up to White Chalk.
Sandstones and shales, with rtf Karoo formation: probably ‘Trias,
shales, and Boulder-bed (greenstone reaching as far up as the Jara.
dykes).
Quartzose sandstone with shales; contain- ? Table-Mountain Sandstone. Coal-
ing only traces of fossil remains. period.
Clay- and talcose slates, mica-schists, dykes
of diorite.
Granite and gneiss, dykes of diorite. Primary rocks.
| Primary slate-formation.
II. Economic Groxroey.
Industry and the fine arts are still in their childhood in Natal;
otherwise the raw materials are there in abundance. Natal possesses
good building-material in the quartzose sandstone of the Table Moun-
tains, and an excellent slate which is found at some places (for in-
stance, at the Umpampinioni river). The lower parts of the erys-
talline limestone would, I have no doubt, afford a good statuary
marble.
1. Graphite—A very good quality of pure graphite is found
south of Springvale, in Natal—in gneiss, as it seems. As the work-
ing of the graphite is not expensive, a ton of pure graphite costing
only about £30, it would probably be a lucrative undertaking to
ship graphite at Durban. Graphite is not very rare in South Africa;
traces of it are found at several points in the “old colony.” A
considerable amount of this mineral is to be met with, as I have
been informed not very far from the Mission-station of Inyatin,
about 20° S.
2. The Coal of Natal, which belongs to a younger series than the
more newly discovered one near Tulbagh, in the Cape Colony, seems
to form extensive fields in the sandstone and shales of the plant-
bearing Karoo formation. Although it is a good steam-coal, it is
still cheaper to import the coal from England or Australia, whence
it may be obtained at 27-55 shillings the ton at Durban.
3. Metals.—a. Gold. Every body remembers the great excite-
ment which was caused by the first “ discoveries” of gold in South
Africa. Since then companies have been formed, shares sold and
bought, diggers have been sent out, and the colonies hoped for better
days; but suddenly the gold-fields turned out to be imagination, as
it became pretty certain, and indeed an ascertained fact, that gold was
not in sufficient quantities to pay the working of the quartz. Notonly
in the interior, but also near the coast, within the boundary of the
colony, gold was sought for. Traces of gold are to be seen in the
quartz-veins and quartz masses (“reefs”) in the granitic and slate-
formation, but not sufficient to pay the expense of crushing. I have
visited most of the localities in Africa which were called auriferous ;
but nowhere did it seem to me likely that it would pay for working,
as the quartz-veins (supposing they would yield a paying quantity)
Quart. Journ Geol Soe. Vol XXVIH' PL TL.
(Gneiss and Granite
RYSTALLINE ROCKS, Clay, maca,talcose slates
Grvstalline limestone
Palaeozoic Formations.
PBONIFEROUS SERIES, ‘Table Mountain Sandstone aa
Mesoxoce Fornvations.
[rats .
AROO FORMATION,
Shales .,
(TRIAS)
ma Boulder-bed .....
SV TACEOUS SERIES, Sandstone
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| COLONY or NATAL
GEOLOGICAL MAP
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1871. Eruptive Rocks.
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CRETAGEOUS FOSSILS FROM NATAL.
1870. | GRIESBACH—GEOLOGY OF NATAL. 71
are everywhere of very limited extent and thickness, and the so-
called “ reefs” everywhere thin out rapidly towards the base; and,
lastly, there is no extensive alluvium anywhere in these districts
which yields gold.
It is a well-known fact that gold has actually been exported from
the east coast for centuries by the Portuguese in large amounts; and
the question may be put, Whence does this gold come? Gold
is there; but the question is, Would it pay white labour or not?
The Portuguese trader in Quillimane has perhaps one thousand or
more slaves, which cost him only a trifle, as they live by their wives’
labour ; when the dry season sets in, the Quillimane traders send
their slaves to their work; they are supplied with old flint-guns, and
sent into the interior to hunt elephants. Some are sent to trade,
and a great part to the diggings in the rivers which flow into the
Zambezi, near Tette, and in those running from the south to the
Zambezi, coming from the fabulous country of Manico. There the
wives work at fields of rice, which support them sufliciently, whilst
the men wash the gold from the rivers in small kalabashes in quite
a primitive manner. As the gold itself has no value to them, they
bring it faithfully to their masters, who reward them with beads
and white Salempore (calico). In this way the master gains a good
deal, as all the gold he receives is a clear profit. If he has only
150 slaves engaged in the diggings, and he receives only 1 ounce
per head in the season, he makes a profit of £581 5s.!_ Of course
white labourers would never find it practicable to undertake gold-
washing there under such circumstances.
b. Copper is already well known in many districts of South Africa,
and is also worked. I found copper at several localities in Natal ;
but nowhere, I should think, would it be found practicable to work it.
Near the Ifumi river, south of Durban, a highly decomposed gneiss
occurs which shows traces of copper at the surface. It is situated
just along a fissure in the gneiss, and it possibly might lead to a
richer point; but this is not probable. In the Insiswa Mountains, in
Kaffirland, richer copper-ores have been known for a very long time,
but have never been worked out. This locality is situated at the above-
mentioned line of greenstone, whieh strikes from south to north,
near the base of the Karoo beds. It is remarkable that along this
greenstone line copper is found. ‘Thus, for instance, it occurs near
the Tugela valley, in greenstone whieh intersects the granite.
EXPLANATION OF PLATES II. & III.
Pzrate If.
Geological Map of the Colony of Natal.
Section from the Bluff, Port Natal, to the Mont aux Sources in the
Draakensberg.
Pzate IIT.
Fig. 1. Ammonites umbolazi, Baily: a, dorsal view; 6, sutures.
Fig. 2. Ammonites rembda, Forbes; a, section; 0, sutures.
Fig. 3. The same, young individual.
Wig. 4. Anisoceras rugatum, Forbes.
72 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Deen7,
Fig. 5. Cerithium kaffrarium, nu. sp.
Figs. 6, 6 a. Solarium Wiebeli, n. sp., enlarged; 6 b, natural size.
Fig. 7. Pecten amapondensis, n. sp.
Figs. 8, 8a, 86. Pectunculus africanus, n.sp.
Fig. 9. Astarte, sp.
Figs. 10, 10a, 106. Arca capensis, n. sp.
Figs. 11, 11a, 116, 1le. Trigonia Shepstonei, n. sp.
Fig. 12. Cardium denticulatum, Baily.
Fig. 13. Diadema, sp.
Discussion.
Prof. T. Ruprrr Jones commented on the importance of the
paper as throwing so complete a light on the geology of Natal, and
proving the geological sequence to be similar there to that in other
parts of Southern Africa. He remarked that the author had done
special service by the great increase of information furnished by
him regarding the Cretaceous rocks of Natal, and their equivalence
to those of India. He also pointed out that Mr. Griesbach had
proved that the Karoo formation was continuous to the other side
of the great dividing range, and formed the floor of the Orange
and Waal valleys, and remarked that as Mr. Stow had indicated
glacial action on the south side of the Orange valley, it was quite
possible that the gravels containing the diamonds were of local
origin, as Dr. Grey had suggested.
4. On the Diamonp-pisrricts of the CarE or Goon Hors.
By G. Girrinzan, Esq.
(Communicated by Warington W. Smyth, Esq., F.R.S8., F.G.S.)
[ Abstract. |
In this paper the author gave an account of a visit paid by him
in June last to the diamond-bearing districts of the Cape of Good
Hope.
Between Cradock and Hope Town there seemed to be no indi-
cations to warrant the expectation of finding diamonds. The geolo-
gical structure of the country between Cradock and Middelburg is
very uniform, showing few traces of upheavals. The rocks are
chiefly sandstones of various degrees of fineness, with alternating
beds of red or blue marl, in hard nodules of which Dicynodon-re-
mains are formed.
On the “ Karoo”: the author noticed that all the springs in that
country rise on the eastern side of dykes which run about N.E. and
S.W. Near Hope Town there are immense tracts of sand. This
village is surrounded by low bluffs of a peculiar rock, consisting of
a calcareous matrix with waterworn pebbles. At Hope Town an
active trade in diamonds is carried on.
The author crossed the Orange River at Hope Town, and describes
the tract of country between that and the Vaal River, called Albania,
as very barren of geological interest, being chiefly a sandy waste,
with a few low hills, dykes of greenstone, trap, &c., and occasionally
1870. | . GILFILLAN—CAPE DIAMOND-DISTRICTS. 73
an outcrop of hard blue schist. Where the sandy covering is re-
moved, a deposit of tufaceous nodular limestone is exposed.
- Crossing the Vaal River at the Griqua’ mission-station of Back-
house, the author entered the true diamond-district. At Nicholson’s
farm, about six miles up the river, he observed the outcrop of a
hard conglomerate, sometimes assuming the aspect of a breccia, com-
posed of angular and rounded pebbles and blocks of quartz, jasper,
&e. of all sizes to upwards of a foot in diameter. Overlying this
was a highly ferruginous soil containing numerous pebbles of quartz,
jasper, iron ore, &c., in which, the author was informed, several dia-
monds had been found.
From Backhouse the author pushed on to Likatlong, about sixty
miles further north. On the road along the banks of the Vaal River
he occasionally observed schistose rocks, and also a great deal of
unstratified limestone, containing quartz and other pebbles, in which
diamonds were said to have been found with limestone adhering to
them. Beneath this limestone, when denuded away, a ferruginous
clay, the same as above described, makes its appearance, and is
searched by the natives for diamonds. The author considers that
the number of diamonds found at Likatlong had been greatly ex-
aggerated. He states that the diamonds were everywhere obtained
from the ferruginous soil, and that the spots which had been searched
were always near the river, and, as far as he observed, only on the
right bank, where the level of the country for some distance from
the river is lower than on the opposite side. He considers that the
finding of diamonds on this side only is due to the absence of the
great deposit of sand which raises the country on the opposite bank
to a much higher level.
Discussion.
Prof. Tznnant stated that he had lately seen as many as 500
diamonds from the South-African fields in the possession of one
person, some weighing as much as 50 carats. He had seen another
fragment of a stone which must have originally been at least as
large as the Koh-i-noor.
December 21, 1870.
Valentine D. Colchester, Esq., 4 Buckland Villas, Belsize Park,
N.W.; H. J. Heighton, Esq., Gold Street, Kettermg; Thomas
Hawksley, Esq., 30 Great George Street, Westminster; Frank
Rutley, Esq., of the Geological Survey of England, Jermyn Street ;
Isaac Roberts, Esq., 26 Rock Park, Rockferry, Cheshire ; Richard
Glascott Symes, Esq., of the Geological Survey of Ireland, of Victoria
Terrace, Ballina, County Mayo, and 14 Hume Street, Dublin; and
Daniel Pidgeon, Esq., F.R.M.S., Banbury, were elected Fellows of
the Society.
The following communications were read :—
74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 21,
L. On Lower Turttary Deposits recently exposep at Porrsmourn.
By C. J. A. Muyzr, Esq., F.G.S.
THE excavations in progress at Portsmouth in furtherance of the
works known as the “ Dockyard Extension Works,” have exposed
to view, during the last three or four years, many fine and highly
interesting sections in the Lower Tertiaries.
I propose to lay before the Society, by way of record, a brief
account of these sections, and of the numerous fossils which have
been obtained from them.
The site of the “Extension Works” lies to the east and north-
east of the existing Dockyard. A description of the works them-
selves would be out of place in this paper ; I shall therefore confine
my mention of them to such points only as may serve to illustrate
the geology of the district.
Previously to the commencement of these works, in 1867, the
ground intended to be occupied was, for the most part, a vast
mud-flat, covered at every tide by the waters of the harbour. The
mud, of which I shall have more to say hereafter, was of the soft
and sticky character so prevalent in tidal basins, and attained over
some parts of the area to the formidable depth of from 35 to 40 feet.
In 1868 the sea was excluded by means of a dam of sheet-piling ;
and the enclosed area has been since reduced, by pumping and deep
drainage, to almost perfect dryness to the depth of 40 feet beneath
low water.
Excavations had been already commenced in the higher portion of
the ground before the shutting out of the sea-water; and in 1867 I
heard from my brother, Mr. C. H. Meyer, that fossils of the London
clay were being met with in abundance.
In the spring of 1868, when I first visited the works, a fine
section nearly 500 feet in length was exposed to a depth of 60 feet.
It consisted of :—
Giraivelyy: osepisich eecd se seseetsae = damnit oneoen purus sat cetaoeniroecan
Stiff clay, with Septaria .....................00
A band of rounded black pebbles in clay
Sands and shell-rock ............:s.seceece ceeeeeeeeeeeceesaee
The fossils of the clay with Septaria were clearly London-clay
species. Those of the sands and shell-rock appeared to represent
more nearly an equivalent to the Bognor fauna; but I was puzzled
by many of the species, and determined to watch the progress of
the excavations.
New sections have been from time to time exposed since 1868,
until in August of the present year (1870) the excavations had so
far progressed as to have opened out clear and nearly continuous
sections of all the strata likely to be seen within the area of the
works.
Description of Strata.
The strata exposed in 1870, exclusive of alluvial deposits, amounted
to a thickness of 97 feet. To this must be added a thickness of
1870.]
about 30 feet cut through in 1868,
but no longer shown in 1870,
making a total thickness to be de-
scribed of about 127 feet (as shown
in fig. 1).
These beds have a nearly uni-
form dip to 8.8.W., or more nearly
south, of from 23 to 3 degrees.
Their rise, measured horizontally,
varies from 1 in 20 to 1 in 25.
Their total rise, within the limit
of the excavations from south to
north rather exceeds 100 feet.
These strata admit of grouping
into four more or less marked
divisions, characterized partly by
mineral structure, and in part also
by a change of fauna. They may
be described as follows, commen-
cing with the lowest beds :—
1. Clays and sandy clays with Uh
JEVAMIESE) @G6ngRbiotidos nocceadboneoe 36
2. Argillaceous sands with Den-
GEIMHIB, canocanbooeesatoqonbo0000%e 25
3. Sands with Lingula ..........0 8
4, Clays with Cyprina and sandy
ClayS ites sdvescssereenret nace esc.
I propose to give in this place
a broad outline of these groups,
reserving to an appendix the de-
tails of the sections and a full list
of fossils.
(1) Clays and Sandy Clays with
Pyrites.—This group includes :—
A. Stiff blue clay ............... 10 to 15
B. Hard sandy clay with Pyrites 15
C. Argillaceous sands with thin
layers of blue clay and grains
and nodules of Pyrites ...... 10
The blue clay of this group was
exposed in a deep cutting in 1868.
It contained masses of drifted wood
perforated by Teredo; and speci-
mens of a large Ostrea, referred
by Mr. Edwards to Ostrea gigan-
tica, Sol. A mass of wood was
obtained to which several of these
Oysters were attached.
MEYER—PORTSMOUTH LOWER TERTIARIES, 75
AMMA OTM MMMM AN aac
(Length 2000 feet.)
aT
c, Mud.
Sandy clay and stiff clay, with Ostrea.
fi MMOMMonMAAcanAMMNnNA TENANT MC
re
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= él aS
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ow Water?
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TA@NOAL |Last 09
76 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 21,
Teredina personata, Lam., occurs in the wood, and traces of a
species of Cliona in the shells of the large Ostrea. A few specimens
of Plewrotoma have been observed in the. upper portion of this group,
but fossils are evidently rare.
(2) Argillaceous Sands with Dentalium.—This group (marked D
on the Section, fig. 1) consists principally of thinly bedded strata of
greenish argillaceous sand more or less mottled and veined with
clay. It includes three or four zones of scattered concretional
Septaria, and terminates above in a double layer of claystone or
tabular Septaria. A layer of fine whitish sand about 5 inches in
thickness runs through the centre of the group and forms a marked
feature in the cuttings.
The fossils of this group of strata include the following species :—
Ostrea flabellula, Lam. Syndosmya (Tellina) splendens,
Pinna, sp. Sow.
*xCardium Laytoni, Morris. xTellina, spec. nov.
xCultellus affinis, Sow. , Sp-
xCytherea suessoniensis, Desh. Teredina personata, Lam.
*Leda substriata, Morr. Aporrhais Sowerbii, Mant.
xModiola simplex, Sow. Fusus, sp.
Nucula gracilenta, S. V. Wood. - Leiostoma globatum, Desh.
—,, sp. Natica labellata, Lam.
striatella, S. V. Wood. , var.
Panopeea corrugata, Sow. Pleurotoma, sp.
Pholadomya virgulosa, Sow. Rostellaria lucida, Sow.
margaritacea, Sow. Trophon tuberosum, Sow.
Pholas, spec. nov. (allied to xDentalium, spec. nov.
Levesquet). * , var.
xSolen (large species). xThenops scyllariformis, Bed/.
sp. *Bryozoon.
These fossils occur dispersed throughout the sands. ‘The speci-
mens of Panopwa, Pholas, and Pholadomya occur in the position in
which they lived, and with their valves united. The species marked
with a star are restricted to this group; the rest range higher.
(3) Sands with Lingula——This group of sands deserves special
notice on account of the number and variety of its fossils. It
includes the following beds :—
HE. Greenish sands with thin layers of clay .....................+-- 5 feet.
F. One or more thin layers of greenish chloritous sand,
crowded with fossils, and resting in places on a thin
ly GiP OE OE ledgoatedaokchlgenge Bocboo.uasbdcanogboconocéaee lto 3 inches.
G. Greenish sand, finely stratified, with one or more layers of
. Shella essa se cee edeck wre nloce pemels weeps slerette reasaatonch odcceaaecuns 3 feet.
The abundance of green matter in these sands 1s very conspicuous.
Concretions of shell-rock many feet in length occur along the
line of sand and shells at F, sometimes including and sometimes
resting on, or appearing to be suspended from, the layer of shells.
This shell rock, which has very much the appearance of Bognor
rock, is so hard as to require blasting.
More than eighty species of fossils, several of which are new to
the English Eocene ‘strata, have been obtained from this group of
strata. A few of these, such as Lingula tenuis, Sow., and Panopwa
1870.]
MEYER—PORTSMOUTH LOWER TERTIARIES.
=
(
intermedia, Sow., occur dispersed more or less abundantly throughout
its thickness.
The greater number were obtained from near the
top of the sands, or from the thin layer of sand at F, where they
lie crowded together, at intervals, to a depth of many inches.
Fossils of Sands with Lingula.
Avicula media, Sow.
Ostrea flabellula, Lam.
Pinna affinis, Sow.
, Sp.
Cardita planicosta, Lam., var.
Brongniartii, Mant.
, Sp.
Cardium (Protocardium) Wateleti,
Desh.
, sp. (small species).
Corbula, three species,
Cytherea proxima, Desh.
—— orbicularis, Desh.
—-— portsmeuthiensis, Edw. MS.
Mactra, sp.
Modiola elegans, Sow,
Nucula gracilenta, S. V. Wood.
striatella, S. V. Wood.
Panopzea intermedia, Sow.
Pholadomya virgulosa, Sow.
Psammobia Edwardsi, Morris.
Syndosmya (Tellina) splendens, Sow.
Teredina personata, Lam.
Lingula tenuis, Sow.
Aporrhais Sowerbi, Manz.
Bulla constricta, Sow. ?
sulcatina, Desh.
Calyptrea trochiformis, Sow.
Cancellaria leviuscula, Sow.
——, sp.
Charani diadema, Desh., var.
substriata, Hdw. MS.
Chemnitzia tenuiplica, Hdw. MS.
Chrysodomus bifaciatus, Sow.
Fusus, sp.
, sp. (small species).
——, sp.
Dee ts eaplenclloes. Desh.
, Sp. NOY,
Leiostoma globatum, Desh.
Murex coronatus, Sow.
Natica labellata, Zam.
splendida, Desh.
pseudo-orbicularis, Edw. MS.
Natica portsmeuthiensis, Edw. MS.
—— subdepressa, Morris, var.
microstoma, Sow. ?
—— lignitarum, Desh.
Pleurotoma helix, Hdw.
stena, Hdw.
—-— (six to ten other species).
Pseudoliva fissurata, Desh., var. ?
sulcifera, Hdw. MS.
Pyrula Smithi, Sow.
tricostata, Lam.
—— Greenwoodii, Sow.
Rostellaria lucida,. Sow.
Scalaria undosa, Sow.
—— (small species).
Sigaretus clathratus, Pec/.
Skenea, sp.
Solarium bistriatum, Desh.
—-, var.
, Sp.
Triton Morrisii, Hdw. MSS.
Trophon tuberosum, Sow.
Turritella sulcifera, Desh.
imbricataria, Lam.
—— Meyerii, Edw. MS.
terebellata, Lam.
Voluta elevata, Sow.
—— depressa, Lam.
—— nodosa, Sow.
——, sp.
Nautihee centralis, Sow.
Sowerbii, Weth.
—— imperialis, Sow.
Flustra.
Bryozoon.
Hemiaster Bowerbankii, Ford.
Cliona, spec. nov.
Palzxocorystes glabra, Woodw. MS.
Xanthopsis Leachii, Bel/.
Rhachiosoma bispinosa, Woodw. MS.
echinata, Woodw. MS.
Nipadites.
Wood (and fragments of plants ?),
These strata have been exposed in open cuttings from one to
two thousand feet in length.
In first looking over the fossils of the “Sands with Lingula,” one
cannot but be struck with the apparent mixture of London-Clay
fossils with species which are usually considered characteristic of
higher or lower formations. The two species which occur the most
78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 21,
abundantly in these strata will serve to illustrate my meaning. These
are Cytherea proxima, Desh.,a species closely allied to C. suberyci-
noides, Desh., and Natica subdepressa, Morris. The former of these,
although not the Bracklesham Cytherea suberycinoides, looks strangely
like it. The latter, a Thanet-Sand species, has not, I believe; been
hitherto found above the base of the London Clay. The same re-
marks apply to several other species present less abundantly in
these sands—as, for instance, Cardita planicosta, Turritella sul-
cifera, T. imbricataria, and others, all well-known species of the
Middle Eocene, while, on the other hand, Cardiwm Laytoni, Morris,
and Cytherea orbicularis, if not strictly Thanet-Sand species, range
elsewhere only into the lowest of the London-Clay strata.
By taking a Darwinian view of the matter, one may perhaps get
over the difficulty of the seeming mixture of species; and this
view is probably correct, for on close examination it is evident that
the common Cytherea of the Portsmouth sands is not quite the C.
suberycinoides of the Middle Eocene, although probably its pre-
decessor, in the same way as its companion shell, Natica subde-
pressa, var., may be the descendant of the NV. subdepressa of the
Thanet Sands.
The condition in which the fossils occur in the sands with Lingula
is also worthy of notice. In the lower portion of these sands, as also
in the underlying “Sands with Dentalium,” the shells occur spa-
ringly, mostly with their valves united, and frequently in their natural
position. Towards the top of the “Sands with Lingula,” where the
shells lie crowded together in layers or patches, there is clear evi-
dence of drifting. The univalves are often slightly worn. The
bivalves appear frequently with their valves disunited, and with the
concavity of the valve turned downwards, as is so constantly the
case between the tide-marks on a flat sandy shore. Fragments of
wood or carbonaceous matter, in minute quantities, are constantly
present in and near the layers of shells*. There can be no doubt
that the “Sands with Lingula” were either accumulated in shallow
water, or as a littoral deposit. .
(4). Clays with Cyprina.—This group includes the following
beds :—
H. Brownish clay, with rounded black flint pebbles ......... 8 inches.
J. Stiff greyish clay with Septaria .............. .....:0eeee 30 feet.
K. Brown sandy clay, with thin lines of sand ......... 15 to 25 feet.
Fossils are far from abundant in this group. The altered condition,
in all probability a deepening of the sea-bed, resulting in the intro-
duction of the layer of pebbles above mentioned, and the abrupt
change from sands to stiff clays, is seen to have been accompanied
by a marked change of fauna. Of the numerous species of Mollusca
occurring in the “ Sands with Lingula,” many of which abound to
within an inch of the zone of pebbles, a few species only reappear
at a higher level in the series.
* Some of the blocks of stone, on being split in the line of bedding, are
seen to be crowded with carbonaceous markings, as of minute leaflets or seed-
vessels.
1870. } MEYER—PORTSMOUTH LOWER TERTIARIES. 79
The “Clay with Pebbles” contains—
Cytherea despecta, Desh. Aspecies Pinna affinis, Sow.
new to the British Hocene. Pecten corneus, Sow.
Panopzea intermedia, Sow. Natica labellata, Lam.
—— corrugata, Sow.* subdepressa, More.
Pholadomya margaritacea, Sow. Rostellaria lucida, Sow.
Teredina personata, Lam. And teeth of Lamna and Otodus.
Of these species the Cytherea is found only in the zone of pebbles.
The Panopee continue their range upwards from the “ Sands with
LTingula” to a few inches (rarely a few feet) above the pebbles, all
Fig. 2.—Beds with Panopeere in position.
a. Stiff clay (J). 6. Clay and Pebbles (H). c. Sands (G).
Species occurring with their valves united, and in their natural posi-
tion. It is curious that the Panopee should have so long outlived
that changed condition of the sea-bed which drove away their com-
rades in the “ Sands with Lingula.”
Cyprina planata, Sow. Teredina personata, Lam.
Pecten corneus, Sow. Pholadomya margaritacea, Sow.
Pinna affinis, Sow. Turritella sulcifera, Desh.
Panopza intermedia, Sow. Natica labellata, Lam.
Pectunculus brevirostris, Sow., var. Rostellaria lucida, Sow.
and very rarely a Nautilus occur in the “Clay with Cyprina.”
A layer of crushed shells of Pinna, an inch or more in thickness,
occurs at about two feet above the pebbles. The shells are so much
decomposed that it is impossible to say whether they were whole
when deposited.
Aporrhas Sowerbi, Rostellaria lucida, a Chrysodomus, and several
species of Plewrotoma occur in the sandy clay (K), which forms the
highest Eocene stratum exposed on the works.
* Panopea corrugata, Sow., is most plentiful in the pebble-bed. I am not
sure that in the sands it can be distinguished from P. intermedia, Sow., unless
by a difference in size.
80 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 21,
Such, then, is a brief account of the strata and fauna of the Lower
Kocene deposits as seen in the Portsmouth sections. It remains to
determine the position which these beds may be supposed to occupy
in relation to the cliff-sections at Alum Bay and Whitecliff. The ~
evidence of the fauna, including as it does many species respectively
of a high and low level in the Eocene strata, is too contradictory to
be of much value. The stratigraphical evidence which it is my good
fortune to be able to lay before the Society, however, is perfectly
conclusive.
I propose to show this in two ways :—First, by comparing the
ascertained rise per hundred feet of the beds described with their
distance from the known outcrop of higher and lower formations; and,
secondly, by the more direct evidence of borings and well-sections.
Evidence of Thickness of Beds by Horizontal Measurement.
I have shown that the rise of the strata along the line of the
section (fig. 1), from south to north, equals a rise of about 1 foot in
every 22 feet. Now the distance from the outcrop of the highest
beds exposed on the works to the known outcrop of the underlying
Red Clay is about 6000 feet, which gives a thickness of about 275
feet to the intermediate beds, or within 25 feet of the thickness of
the London Clay and Bognor series of Whitecliff. Then, again, the.
distance from the line of strike of the higher beds on the works to the
nearest known outcrop of the Bracklesham beds is about from 6500
to 7000 feet, giving a thickness to the intermediate strata of from
295 to 315 feet. And-this thickness agrees very nearly with that
of the Lower-Bagshot strata at Whitecliff. Supposing these measure-
ments to be correct, the strata above described must represent nearly
the upper portion of the London Clay of the Whitecliff and Alum-
Bay sections.
Evidence by Borings and Well-sections.
The thickness of the strata exposed on the works in open cuttings
I have shown to amount to about 127 feet. A boring has been recently
sunk from almost the lowest of these beds to a further depth of about
115 feet (fig. 3, 6). The details of this boring are as follows :—
Details of boring in Extension Works. f. in,
Samebyy clan i iter cetacacee teases tena eeeuine seeremeeits 10 0
D With more Clay ........00ce..-20sessesseeeeeree 5 O
Stith clay. Weaguicen taccmuccee sua emese cases: ate se csecheeeerere oO
Very stiff clay (=‘‘Clay with Ostrea” of theSection) 18 0
@laystome chee EES SE, De NSE ois SER eels 2
Woery: stitticlayy anitin, c it eds Acta aad da aiecn ee eemeae 29 0
Layer of Pyrites anda small shell (Zurritella) ...... 1
Stitiiclayeescseee eee de ao eres Use ala eisai « secleloee eee 12 8
C@laystone seek vee eonseln races ee Sebipaikte sac aale eee 2
(OL En qin a san dans eg deena EES oy Tit amen n Sate AMAEEE REE d.o0 500% 2 0
Claystome ci. 3. sritin wa coetigticn- tek « «aie ws) eteas CeeERME 2
Werty stitt clay i sccai ees sont eer ia cine) ieee 10 10
Clay full of rounded black pebbles— .................5+ 9
Hard pam: (ih Scat Pa ita te doeists seo vgs gee Ae Lane 22 3
Bluciela yeuise set eeeecetns gaan ease ear ans ctic eet ceiter eee 39 0
ic
a. Whitecli}
Hard ferrugi-
nous sand. ft. in.
20. Bay
2
(=)
=
cy
®
ind
a
=
S
5
=a
36 0. Stifl
18 0. Clay
.. 4 6. Clay
SSS... 1 6. Indu
180
=—..-14 6. Clay,
170
: ---12 6. Clay;
fey =Tabann6 Laye
——————— Pé
}-22 0. Stiff!
So 0 6. Sept
SSS
lcd elay,
about 140 fret.
[To face p. 80.
e. Section of Deep Well, Portsmouth Dockyard.
Surface.
Grey, brown, and yellow clay.
Brown clay and sand.
=| Blue clay and sand.
‘Light brown clay, very sandy.
Brown sandy clay, and thin layers
of stone.
. Blue clay, with pyrites and thin
layers of stone.
Blue clay and pebbles.
Sand and pebbles.
Hard stone.
‘Fine sand, very hard.
Hard stone, with shells and fossils.
Fine sand.
Alternations of blue clay and sand.
Blue clay, with thin layers of clay-
stone.
Mixture of blue clay, sand, and
|| mottled clay.
Red clay, 118 feet.
Fig. 3.—Comparison of Section at Whitecliff Bay with Borings at Portsmouth.
a. Whitecliff Bay. b. Section in Dockyard Extension Works, Portsmouth.
Hard ferrugi-
nous sand. ft. in.
0 = = 2 0. Band of ironstone, runs out on
== beach.
20
+30 0. Laminated sands and clay. |
10 .
ty)
5 ——<$<$<—<—<— |
14 0. Hard sandy clay. Surface.
300
_———S .
eS Flint gravel.
Surface.
fs 0. Stiff sandy clay, with Septaria. 290 Bese
Sandy clays 280
. Sandy clay.
0 6. Black flint pebbles... AW ioe) 270
16 0. Laminated clays. Clays with . Stiff clay, with Cyprina planata, 260
_ Cyprina. 5 peter corneus, Sc.
———SSS]}... 8 0. dy clay. assy . Septaria. 250
SSS Bandyiclay, Pebbles Sates, Zone of Pinna.
Sends, aaie i . Layer of rounded black pebbles. 240
Lingula. . Sands, with shell-rock. ES
+30 0. Clay, with Cyprina and Cytherea. 20
290 i Argillaceous . Argillaceous sands (mottled).
| sands, with . Kine whitish sand. 220
210 J . Dentalium., . Argillaceous sands.
) : . Iron-pyrites. 210
200 (18 0. Clay, with Qytherea. vein cayepHllnecton ae ca
——- Bandy clays,
¢ . 46. Clay. . and clay 9 . Sandy clay. 190
=>}. 1 6. Indurated clay, with Cyprina. with oysters, *
4
..-14 6. Clay. 180 Brown sandy clay, and thin layers
of stone.
170
-12 6. Clay, with Cyprina. iff clay.
SS etoue Layer of dark green sand, with Sey, 160
Panopea.
=--22 0. Stiff clay, with flattened Septaria. 1D
— 0 6. Septaria. a . Pyrites. sine cay ath pyrites and thin
Sa... 3 6. Clay, with zone of Pinna. oo 4 eae layers of stone,
6 ; z ts pi i
SS 8 6. Clay, with Panopea in position. 8 rs Go eae Hess isa ines ;
Zone of large oysters. | 120
Pee sees S cnareneee ete sete tales S Very sliticlay,
panics Pebbles .........5 . Rounded black pebbles, 110
= oP ===! Blue clay and pebbles
a tah SS SS ls
3 Hard sands f “100 Sand and pebbles.
2 Hard stone.
3 90 Fine sand, very hard.
80 0. Hard sandy clays and sands. a
80 Hard stone, with shells and fossils.
| Blue clay. ma Fine sand.
Alternations of blue clay and sand.
60
0 6. Septaria. 50
Bottom of
boring. ; 40
Blue clay, with thin layers of clay-
stone.
38 0. Sandy clays, with few Septaria.
20
0 6, Sandstone, with Ditrupa. ° i —————=——————
4 8, Dark greenish sand. j SSS Hj==|| Mixture of blue clay, sand, and
0 4. Conglomerate of small fragments 5 0 eS _ mottled clay.
Wd clay, of grit and red clay.
Red clay, 118 fect.
about 140 f. et,
En Ewa VEIN crt
fae iy 2
BO tan
ue
iene yy
" Rhee, Leva eins
ii Ea RENTSE A Bea ape
Hl Nea Sete eh ae. Ae g
1870. | MEYER—PORTSMOUTH LOWER TERTIARIES. 81
The point of chief importance in this boring is the occurrence, at
93 feet below the lowest beds exposed in the open cutting, of a
band of rounded flint pebbles, similar to that at the base of the
“Clays with Cyprina planata.’’ The discovery of this second band
of pebbles has given a clue to the position, in relation to the under-
lying Plastic Clay and Chalk, of all the strata seen on the works,
as I shall show by comparison with the records of two previous
borings in the Dockyard.
For permission to avail myself of the records of these two borings,
which probably have not been hitherto published, I am indebted to
the kindness of Mr. Wood, the Superintending Civil Engineer at
H. M. Dockyard at Portsmouth.
The first of these, known as the Deep-Well boring (fig. 3, c), is
situated at the distance of 3000 feet from the boring on the Exten-
sion Works, or only about 170 feet 8.S.W. of the line of strike of
the highest strata above described. It was carried down to the depth
of 1037 feet. In this boring the chalk is reached at the depth of
408 feet. The thickness of the Red or Plastic Clay amounts to 118
feet. A layer of rounded flint-pebbles is shown at the height of
100 feet above the Plastic Clay, or about 190 feet from the surface.
There can, I think, be no doubt whatever that this pebble-bed
represents the pebble-bed cut through in boring on the Extension
Works. It is curious, however, that the upper pebble-bed is not
shown in the Deep-Well section.
The second boring (fig. 3, 6) im the Dockyard (the first, perhaps,
in point of date, as it was made in 1825) is at the distance of nearly
1000 feet 8.S.W. of the line of strike of the highest beds on the Ex-
tension Works. It has been carried down to a depth of 290 feet.
In this boring both the pebble-beds are shown; and the interval
between them corresponds exactly to that between the two pebble-
beds on the Extension Works. The same beds have been also shown
to occur, in the same relative position, in other borings at no great
distance from the above, as well as in well-borings through corre-
sponding strata at Southampton*. ‘Two pebble-beds are shown by
Mr. Prestwich as occurring in about the same position at Alum Bay f.
It is shown, then, by the evidence of these borings as explained
by the open cuttings on the Extension Works, that the strata there
exposed range from the height of 163 feet to that of 290 feet above
the Red Clay ; and by the same evidence the position of the re-
_markable shell-beds underlying the zone of pebbles and “ Clay with
Cyprina”’ may be placed at the height of 233 feet above the Red
Clay, or within from 60 to 70 feet of the base of the Lower Bagshot.
[Note-—The term Red Clay here made use of answers to the
Plastic Clay of most authors. |
Taking now a more general view of the London and Bognor strata
of the Portsmouth district, we find :—
That their thickness certainly exceeds 290 feet.
* For details of the Southampton well-borings I am indebted to Mr. Bristow,
of the Geological Survey.
+ Quart. Jown. Geol. Soc. vol. ii. pl. ix.
VOL. XXVII.—PART I. G
82 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 21,
That this 290 feet is composed of a threefold series of strata, the
lowest of which reposes on the Plastic Clay.
That each division of the series commences with a zone of pebbles,
and passes upwards from stiff clays to sandy clays and sands*.
Of the lowest series nothing is known with certainty, except its
thickness (100 feet) and the mineral composition of its strata, as
shown in the Deep- Well boring.
Of the middle series, which includes a thickness of 134 feet, a
large portion has been seen in open cuttings on the Works. It in-
cludes in its upper part the “Argillaceous sands with Dentalium”
and the ‘‘Sands with Lingula,” described above. ‘The shell-rock in
the “Sands with Lingula’”’ at the top of this series probably repre-
sents the Bognor Rock of Sussex; but of this I cannot speak with
certainty, as I have no evidence of the height of the Bognor Rock it-
self above the Plastic Clay.
The upper series, having a thickness of from 50 to 60 feet of clays
and sandy clays, including the “ Clays with Oyprina,” has been suffi-
ciently described above. There can be no doubt whatever that these
last beds represent the upper beds of the so-called London Clay of the
Alum-Bay and Whitecliff sections. It is evident that the whole
of the strata above described are included in group 3 and part of
group 4 of Mr. Prestwich’s Section of the Whitecliff strata.
The accompanying Sections (fig. 3), which are drawn strictly to
measure, exhibit a comparison of the Lower Kocene strata of Ports-
mouth, with the already well-known Section at Whitecliff Bay,
and may, I hope, be ultimately useful for comparison with a much-
to-be-desired well-section at Bognor.
Thave not thought it necessary to compare the Portsmouth Lower-
Kocene strata with those of the London basin, such comparison
in effect having been already made by Mr. Prestwich so long since
as 1847,
Gravel- and Mud-Deposits resting on the Lower Hocene Strata.
The superficial deposits seen in the excavations at Portsmouth
deserve a short description, if only on account of the fine sections
exposed.
The first or oldest of these deposits is the gravel-bed shown in the
Section (fig. 1) as capping the higher portion of the ground. The
base of this gravel-bed stands at from 15 to 20 feet above low-water
level, and rests on the unequally eroded surface of the clay. It is
a light-coloured subangular flint-gravel, and probably represents
the “white gravel” lately described by Mr. Codrington}. The
ground on which it rests forms a low escarpment facing to the N. and
N.N.E., the direction of the escarpment coinciding with the outcrop
and line of strike of the upper beds of the “ Clay withCyprina.”
A few patches of contorted gravel containing large, partly rounded
flints, have been exposed at a slightly lower level near the edge of
* A like sequence in the mineral character of the Lower anid Middle Hocene
deposits in the Isle of Wight has heen noted and commented on by Mr. Fisher
(vide Quart. Journ. Geol. Soc. vol. xviii. p. 65).
t Quart. Journ. Geol. Soc. vol. xxvi. p. 535.
1870.]} MEYER—PORTSMOUTH LOWER TERTIARIES. 83
the clay escarpment ; but their relation to the principal gravel-bed
has not been clearly shown.
Passing from the gravels to the deposits next in age, we come to
various beds of silt and silty clay underlying the most recent mud-
deposits of the harbour. These beds have been exposed in clear
vertical sections many hundred feet in length. In all of these
sections the underlying Tertiary deposits are shown to have been
cut away to a smooth, if not always to a level surface, the depth
to which they have been eroded varying from a few feet above low-
water level, as along part of the general Section (fig. 1), to that of
from 20 to 30 feet beneath low water in the north-west portion of
the area.
The surface of the mud over the whole area stands at from 6 to
7 feet above low-water level of the ordinary spring tide.
The following section (fig. 4) exhibits the principal features seen
in these deposits.
Fig. 4.—Ideal Section showing the Relative Positions of the Gravel-
and Mud-deposits.
x. Gravel.
A. Old mud-deposit, with stumps and roots of trees.
B. Recent mud-deposits.
C. Shingle.
In this section the gravel-bed, marked x, and the older and
newer mud-deposits, A and B, are shown at their relative levels in
relation to the present high and low water. It is not improbable
that this section, which represents only a very small portion of the
great mud-flat between Portsmouth and the foot of the chalk
escarpment of Portsdown, may serve to illustrate the general con-
dition of the surface-deposits of the harbour.
There ean be little doubt that the gravel-bed (x) was at one time
continuous over a great portion, if not the whole, of the surface of
the harbour now covered by mud or water. At what time or in
what manner it was denuded I shall not stay to consider ; it is suf-
ficient to know that the denuding agent, whatever it may have been,
has cut down to the underlying sands and clays of the Kocene-
beds, which present, in all the sections I have examined, a cleanly
swept surface beneath the mud.
The older and newer mud-deposits, A and B, shown in the
mud-section (fig. 4), were probably formed under very similar con-
ditions. The bed A is first seen in the sections at about 300 feet
from the low gravel-capped escarpment, and spreads out northward
‘and westward until cut off, as it were, by the deep water along the
G2
84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Dec. 21,
Fountain Lake. It rests everywhere directly on the Eocene sands
and clays; and its lower beds are in a great measure made up of
these underlying sands and clays re-deposited. This is so much the
ease, that it is often difficult, even in the open cuttings, to distin-
guish between the top of the Eocene and the bottom of the mud.
Change of level, or possibly the silting up of some narrow inlet
to the tidal water, must at some time have converted this mud-
deposit (A) into a land-surface, as its surface, where not eroded, is
seen dotted over with the stumps of trees of small growth—possi-
bly Alder or Willow, their roots often penetrating downwards
vertically to the depth of 5 feet. The present surface of this root-
bed stands at from 3 feet above to 2 feet beneath the present low-
water level of the harbour. It is this root-bed, probably, which
has been described by Sir Henry James* as occurring beneath the
dockyard at a depth of from 4 to 14 feet beneath low water.
I do not see exactly in what way to account for the difference
of level of the root-bed shown in the Mud-section and again
beneath the dockyard, except by supposing a subsidence of the
underlying Tertiary deposits. It is at least worthy of notice that
the dip of the root-bed in this area corresponds in direction with the
dip of the Eocene strata on which it rests.
The mud-bed B, or recent mud-bed as it might be called, as com-
pared with the root-bed, commences at the foot of the low escarp-
ment, and, spreading northwards and westwards, rests everywhere
directly on the Hocene, or on the mud-bed A where this is present.
The surface of the mud (B) stands at from 6 to 7 feet above low-
water level, or just midway between ordinary high and low water.
One may suppose, indeed, other conditions remaining the same,
that this level would be indefinitely maintained, the flow, and con-
sequently the carrying powers of the water on and off the mud
being equal. A study of the sections tends to confirm this idea;
for there is evidence in these of very slow deposition near the sur-.
face of the mud in most places, and of very rapid deposition in a
few others—the rapid deposition, as along the edge of Fountain
Lake, being clearly the result of silting up to a certain level.
The spread or overlap of the mud-bed B so far beyond that of A
seems to point to a cutting back of the gravel-capped escarpment,
for the same distance, since the submersion of the root-bed.
The gravel-bed w contains no fossils.
The root-bed contains rarely a few specimens of Littorina.
The mud-bed A is crowded with recent shells at and near the
surface, and usually also near its base. Antlers of the Red and
Fallow Deer have also been met with in this bed.
Thin beds of fine subangular shingle are seen in places, either
interstratified in the mud or near its base, and in all cases include
recent shells.
It has been my good fortune while studying the above sections to
enjoy the friendship of several of the gentlemen in command of the
works; and to their assistance I am indebted for much valuable
* Quart. Journ. Geol. Soc. vol. iii, p. 249.
1870. ] MEYER—PORTSMOUTH LOWER TERTIARIES.
85
information, which would have been otherwise unattainable. My
thanks are especially due to Mr. Edw. P. Smith.
To Mr. Edwards, Mr. Etheridge, and Prof. Morris, I am largely
indebted for their kind and valuable assistance in the determination
of the fossils.
Table of Fossils from the Lower Eocene of Portsmouth.
el. |e 128
eile ES(s
Pasa /ESle8
OS|™ 8) ais | a9
xi x oS Nn
LAMELLIBRANCHIATA,
(Monomyaria).
Alynieully Tage heyy Slada ie sepstodcbeguoodssooobednoodnsobSKodlbane bseob" jobondc r
Ostrea gigantica, Sol. .........ceeceseensceseeceereescesereen|eerene|eccenc|encera|shawen
= tinal, JOG70s) /eantocooneoeocsbcacseabscecodsadapsopedecs obsaue sdoses @ || ie
Pectemkcormeuss SOW. !. oh: sacs cccdscsuctece sense coaeacen se Yr Yr
Bina eDRAT MAS SON Macaca sisi alchineerieescecaseciecaeareecies c Yr ip :
HUI AES [kee ca caien tus wacwacceess ssi sascesioa ieee peodongooopaocaalls 50009|fo05000 ||
(Dimyaria).
Canditasplanicosta, Lam, var. aceeeseceescnsssscenesesece|eraee-\ee- ee r
== LOT, CKO. Se canpeaeron hoedboAnenooceceoLpba eer josd00d| sn000 c
San SD: (Smnalllvspecies) iesceensecserene-asce tasseseeeceesse eas Susie osha r
Cardium (Protocardium) Wateleti, Desh. ...............|ecc0e-feeee- r
== (30) (GimAMIL | MeCHES) ):e sosogoaeddodoocncodnaducsousoncasndbace|ooeced aocbos r
=== Dat AiO, AUCZAUS opiaso doe vbcob sooubbnb bbdcdl ae aeadodensde||son8be| sadder [>ob0b5 c
Corbula Morrisii, Hdw.,Geol. Journ. x. t.2. f. 1, low. fig.|......]...... r
==) (CIDY. | Bebe ao sad aSsoa aan BoR ono cE coos ado ssarncossecrcocoreocal Aascca lsudrsc Yr
Fee PISWINy| SOW: Weenies a doeeaan Gus MAURIS LOAE SERN ee oaEA NA GaInc eR eedel cd eR RRAe r
Cultellus affinis, Sow. .......0.:c.ce-ccceccscnececaeees Seen Rca amet ens c
Cytherea proxima, Desh. (pl. xxx. figs. 31-34) .........[...0.-[eecees c
— orbicularis, Desh. non Hdw. ....c.ccceccccececcecsesecs[eccoee|eceees c
— pseudo-orbicularis, Hdw. MS. .........seeceececcecees[ecesesfeneees r
— portsmeuthiensis, Hdw. MS. .....:.... ocidan0006 hopodboe||acco0allooocce r
Sa ISTICSSOMMOMSISHMIES/2:.3:-) nen ene camer semainentacseenteaseee|steaenienst os [aasees ec
— despecta, Desh........ jatsiate diss tuelh etnies ih eaieer ens Saasueaaeeleasis ec
Cyprina planata, Sow. ............seosssseereee dsanaocadoonad| G
Leda substriata, Morr............+s sauehadiasaee aes REE SSE an eel Seatac c
JWI YO es {57 Ose doaaosaoneenssnagdadareensdsecbustaddoncAnedaddannnd lnnaaes enacas r
IMMoxe Hoke Tiana ese, OCT coongconsegsoscscaaccaacooHuocodeanoued|coods.||auadballaacoee r
== GgeaMs, SCA; ocossanacasadondgosaosan0 Adeased wesccsdoaecoo poses Ooodes r
FSS e eas aectcmanatas detec ae caneenenn ee SeueMeECeAnOe SME ER OEE meEle Hepidd Poradel aaeend r
Nucula gracilenta, S. V. Wood ...........c.cesesceecnceec[eeceee|oonens @ |e
—= striatella, Si Woodsen ey ee ene NY UTR HE r|e
tS) | RP aCe anise noc Hane comes Bontioecericccanpe: ctor creme sac Nee ficn Pecan iwene r
Panopeea corrugata, SowW..........0.cscesencssececoesecnscecaleceees @Allassooe r
= Tirnere aac bi, SOU, scgnoodocsonscedonndednececonseodbbonaonne r r c
Pectunculus brevirostris, Sow..............secesseccseeccvee c
=—— Gecussatus, Sows! */\.Maieesruarnee nessun uc suurchaseocolanweccl ss ttine ealeecn ee
Pholadomya margaritacea, Sow. ............sceseseecneoees (chan fis hoe apes r
Se Ne UlOsas, NOW.» sahesameeneemmesntcnscesse eres se ct|tdeses le aeuee me) |)
TPINOIEISy BS) Oe ised bandsacecasecondsceccovomsdarasosearddacced lieenba Hadund decade r
Psammmobia Hdwardsi, Morr. .............cecececceeececlecceeeleceses Yr
Solen, sp: (laveeispecies) 22202. <seeasoccs sca cieecaseeeecncelsesees|neotcleee cs: r
1. Clays with
Ostrea.
86. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
LAMELLIBRANCIIATA (continued).
Solen, sp. (small species) ...... sbslininsrebiaoes sade stores
Syndosmya (Tellina) splendens, Sow. ...............+65
Tellina, spec. NOV....+0......-.. aisles Waele eeefoee aibiemtaneeretaerse
Hp SPo cere eceereseccereressseces Ooosecsacccs Hasaqoonsnacsskanos
Teredina personata, Lai. ......-.-...c0ceeeveees nce bane
BRACHIOPODA.
1D yaYETRUKE) (HEYMIUIS, SOB so.co¢ pp socoonsnascaenbsosssoqbooecoecooe
GASTEROPODA.
Bulla constricta, Sow. ? .........sceccceecescnes eee seceeees Seta
—— sul catinan Desh. boric. Nestsaas arias uaa vali Levee ea iaill male
Calyptrzea trochiformis, Sow. .......... phosuboaunacanbosnos
Cancellaria leviuscula, Sow. ..........00...csceecsecseeees
pore) sp. eee ecev ce SSccccsesoocerg eeccccseses eoecoscsaretevevccess eee
Cassidaria diadema, Desh. ......ccecscccsceccceccorceeeuee
<a imate VEU latte cielo s etal (olieitelelee Uetsis wceleisale setelsa eins cee maaeines:
— substriata, Hdw. MS. ...... Sacilsiaetincamatste Sslanienive Sooolloos
Chemnitzia tenuiplica, Hdw. MS. ............+ Ss aeaiedysc
Chrysodomus bifasciatus, Sow .................seeeeeeeee
mah E)on' asoaad aids Rae al actu iaerrele Rete au Relate deme est
TENURE, REWEIENL NAGS, Gooaooooucendercocaunodobodsdbooseb0sbe
Leiostoma globatum, Desh. .............cececceetecneceerees
Murex coronatus, Sow. non Born ........-...sec0eceeeee
Isenetee Jeplolllend), LGI70s qocoospboadbocoodeondbododegonoecoonste
Sey EIS UR GENS RSI Suet AD he re ‘ioe ease
oo fe }8) (ea TOE DAV ON SAN Anlsheshaeccissapecbaue sear ac deecasuaces
Poa Paar ab sie 0/0) mace reeeconeeobeen queued sedunneccoacten
HS SUlodls ness VIO ViRTE, ohbgassnoundadanadodsdasoee0e:
> THANE ROS OHIO, LOUIS 1 caeonnoonbongacdecdonacbnouanaussousoo.
— portsmeuthiensis, Hdw. MS. ... .......2..22.s2c--coee oe
Pisania, spec. NOV ............+ pocriocennasens Honbhoaddaceebe
——sublamelllosa, esis oks vane ws alias cheng wane eOaunee
Pleurotoma helix, Hdw. ...........0.....ceccceceeeeeeee eee:
SS HSLCTLA, WELLS, wien eine i AOR oe ne GAR Ey eta ta
== terebralisy Tamealy sis. waneuendee jeans menue aera di
Ha EXQUNIMIGOE NEG (SICUIB) decunnenessestsacouas deka guapeenacacc score
—teretriumy, Haw ela acs suaeak ooee co couanetec aaa
Sar LLGTIK OL JOLIE Gar edurhebakaneutbocuouedbasocedecsabhecc:
mart OMOLAL SPECIES: Meecennssuse Used dene aetna cH ame eel ics
Pseudoliva fissurata, Desh., var. ..........0.0.0ccececeee eee
fear teva JuiKap, JWUSK WRN AA Akane heey hacen aan Se
Biyrailay Sinithiit yy Sotus casey eceensceeeccee-e Peo eee pees
== PI Costa ba Ease asses saen cnc o suo deke te vos ceases eeeneneee
| —= Greenwoodil, SOW 60). .cccccesseeceesnstscsecoecescedoees
Rostellaria lucida, iSo7u e seeds eeeeeencesseeee ee eee eee
SS SES VBR, ASE AU Pa ARO MRE ELAR yer BO 1 (2-
Scdlaria undosa, Sow: sadsse eens eee eee eee
Cyprina.
X Pebble-
4, Clay with
bed.
were tl se eeee
wee teelewsoee
sececcloaeces
ee ceeelecceee
c ie
[Dec. 21,
ESIES/| ES
gs /gs| es
BS) eS | es
aN |/aQ}OO
oS a a
1870. | MEYER—PORTSMOUTH LOWER TERTIARIES, 87
aon et ee
BAe |ESIESIE.
Ss asia 3 8
Ba|Sg/e2| 22 | BS
OS| TS) aN /2Q (5S
Si) pee ieee Wes
GASTEROPODA (continued).
Scalaria, small cancellated species ...............:e0eeeeee[ecseca[eeeees r
Sigaretus clathratus, Reclwz (canaliculatus, Sow.) ...|......].....- r
Sem eais sees tse esses cee nsalseh scence ep eenealstmantaciasseisneel tate Mubiads r
Solariumibistriabum, Mesa). -c--p sess es seccscecessee scales sane eeene c
Se UTE SCRE RCRO TENE GAO ORC ROCCO SCRE INE Ee UEC anCe lee! el lara r
ee SOMME Ce tite Hecht cin dahld seatieivies Sec tes cui re veasemcesecmeme| vcore SeOake r
Triton Wires Jn, WIS sscaqsnanccxancoonosoocusseabeosdl lose nn lacoone r
Trophon tuberosum, SOW SMe .crisiorewiatisiacunaenctua shies Manes eee MoaneE rj/r
Turritella sulcifera, Desh. .......ccceccceceeceenesnceeeees wa aee r
= MIMI CALAT APA seca ounces ciclasiacichnaiee Gee caiawiasins cmactel Ye ccioc| Wace s Yr
25 (Wome oralll Phy W577 Oana a Oaeua wan obeac an coooacneceaatetencerone astanclictac: r
cae UOMO TN PIA LUIS oi Ais Seraiuoectanatiewiesrmeneinene aha seae le SLC r
Iolittayelevabacy SOW cen iciflie wsecninceositamecsaceeetweeaene Seem lpacee c
HCPL CSSA LAO! «woth sacieMes Seas ot sinsineismesbaciins <adettasedlemasnatae seed r
ATT CCL OSEUMISO CUEN eaters ele ss tincis corde Su cIe SIR GCS nSeio ments een a wtatal one Bac onl r
SEES ase se omaaae dat aan toa nt emiemenuterninecieeaenence satel cease euel r
IDierantalliniral, (yl LOWS | Soadanpanadeondseosdocbucaeedeeodasbodel|, pica ssaead boddaa c
PUNT Ns Ste cack cfceiava ware ici ies Saeofe a ater to silane cleats Sarees Micke ie mag ses] ee lads Ze r
CEPHALOPODA.
Nautilus centralis, Sow. ............+. Sane RAH AHH SSDS ACE aaa Pa eee r
==> TANT ISCAS Bericaseancetoncsde oodshoadsanucendadteeds re ual eats r
== NOWErDI, Weta 2. hock cscs ede vns cacecucuseslovelraalnlleds!s'ss regal Reset r
Bryozoa.
AES EVOZO OWE eRe ee co sc diciece uaa ten Hue siauan een ne sebaee seomeasled| eek oa) eMban r r
Vas trrengeeee occ sas asacueeeen aes HEA. See Ren Muse Fair Mestad r
HcHINODERMATA.
Hemiaster Bowerbankii, Forbes ....0....cscceceecsecseserel.ceccleccees r
SponGiA (AMoRPHOZOA).
Chigria sep mn OV ilies cb Laratcn ToMee ote me tees ec aelteelo wen cess (il tan! jr keene r
CrusTACEA.
Paleocorystes glabra, Woodw. M6....... pee eaaceenleisisi Eee he r
Rhachiosoma echinata, Woodw. MS. ............ceesse00-|,....-leeeee r
== ly ONORE [OCCKIWISS | sascacbuabocbocossede dacdoadsadudl isaeaslbssoss r
Thenops scyllariformis, Bell .............0--02-eseeceeeee|e-occeleceeee Bocond|| 12
Xanthopsis Leachii, Bell ...........0...+06. dpanoosdadond s00|| 152 Iloaboac r
Pisces
Lamna elegans, Ag. ............+ GB UOSSEE ASB SoSH SHE SoBe OH GeOEE| ARR r
Otodus obliquus, 4g. ............ Upiaciicr sagcsiessicasiaeetiste esl ics eMhib5y
Sauroid toothy) 200.4... irasectactenee seetnecaenoee saceanieclesiellasisns lee eisten r
Werfebree) (Of fishes) ..sreweeccncnaeeterencercesesn sec shoace|: spsag|aoasas] FP
MivAT@ DALES NSD slastesisciioisoetesniscesese sii siie seer a ewocionecal eee waclic
PLANT.
Nipadites, sp. ............0+- Beacon pov ondaogocpnootcebHd Sod boonad|lcadoadll | #2 ;
WiOGd eicosicsencecensssscesesclecses SUdanbod GUS SB ere Ces ES OSEHOHS oncoe) iP || c
88
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
APPENDIX.
(Dee. 21,
Details of General Section of Lower Eocene deposits at Portsmouth
(Dockyard Extension Works), commencing with the highest strata
‘Pebble
feet. inches.
exposed.
& ( Brownish sandy clay, with thin partings
us) ofisand ei te cee oree sate Pr esinaccan tact 25
bm
iE [eaepeas CLAY: nuisnocuecsedaaate seasommeneeemrene 9)
w \Sand, with small nodules of claystone... 0
Brownish sandy clay .............00.000000+- 4
SOM tAM1A, Heim ataccts estes dsacesanacsaeteatoeens 0
Browmishiclay ans. sossvene sees seeceeesee sane 9)
| NEPbeilay 0 eats lake muecearuavanerareneeee 0
Layer of greasy clay .........-.-0s0e0.c.se008 0
s Stiff greyish clay,with thin partingsof sand 5
= Sand, with pyrites ...........e..06 prowoancee 0
S | Stiff greyish-brown clay ........--....-+6-++- 2
2 Septariay ce-tccesutenessensserusreses see eeeae: 0
3 Stiff greyish-brown clay...............-++8+- 5
Pa | andy; clayy tis. ice cannescasacceeeun Cour eeeeee 0
GS Stiff greyish-brown clay ...............-.-... 2
bed.
|
|
i
:
Sands with Lingula.
Argillaceous Sands with Dentaliwn.
|
Thin layer of Pinna; crushed, and much
decomposed. (These shells appear to
have been whole when deposited.)...... 0
Thin seam of greasy clay .......0......... 0
Stiff greyish-brown clay..................... 2
Brownish clay, with rounded black flint
(DELS) (BE noa4ooansooqnosnbondoontoscqboacoee. 3 0
Greenish sands, finely bedded and inter-
stratified with thin lines of clay and
fragments of carbonaceous matter.
Fossils numerous .......... gocbudocs0s00¢ 3
Layer of greenish chloritoussand, crowded
with fossils, and forming the nucleus of
a zone of large concretions ofshell-rock 0
Argillaceous sand, slightly mottled ...... 5
Sand, with double band of tabular Clay-
stone or Septaria, containing thin lines
of vegetable matter ........0......c00see00s 1
Greyish-brown (or greenish-brown) mot-
tled sand, with thin seams of clay ...... 6
Septaria, at wide intervals.................. 0
Greenish-grey argillaceous sand, mottled
and veined with clay ..............s.c0e0 4
Layer of finely laminated sand, nearly
white when dry ..............seeseeeeeeees 0
(This bed is very constant in thickness
within the area of the excavations.
Greyishargillaceoussands, slightly mottled 4
ISIE} La 2 hash coder postedadndbdddosdcansdeneeteod
0
Greyish argillaceous sand, or sandy clay 5
O Zone of Pleurotoma
(several species).
Zone of Pectunculus.
WNoOndooWP
Zone of Aporrhais
Sowerbz2.
Zone of Cyprina
planata.
a
10 Zone of Pholadomya
margaritacea.
2 Zone of Pinna.
1 Zone of Panopea.
10 Zone of Cytherea
despecta.
0 Zone of Panopea in-
termedia.
1 Zone of Cytherea
proxima, &e. &e.
6 Zone of Pholas —.
5
6 Zoneof Cardium Lay-
toni and Cytherea
suessoniensis, Desh.
6
1870. | MEYER—PORTSMOUTH LOWER TERTIARIES. 89
feet. inches.
& (Thin line of sand, with pyrites ............ 1
& 4 | Thin band of blue clay .................0065 4
a Hard sandy clay, with thin lines of stiff
aa GER? Gacnecadcon: angaebodoncebas cocoooeaccas0n0 10 O
&q | Ditto, with more clay.................0s20008 5 0
3) 42) || Simwit PEA coccoono5sqebedoceoacss 1c sagseccooscacc Bw
B F | Very stiff clay, with large Oysters......... 18 0 Zone of Ostrea gi-
3S) gantica. _
(( CHES SHOES nAgh saedocgedecucoce ep Aadiocboecusece Oe2
& Weieyy Cm GENT. cooddecasoaccanconsspaseano0I. pe AS) AAD)
2 Bayerofi pynites <. 22... -2.-crsec-cssescee see 0 1
2 ei] (SHU Gly, desgebocensdaneeoboseac uses coor -ecoee 1258
eo eNO AV SLOMC ag. cena seerasion sess. celta cence. sie e cate 0 2
#36 4 Clay ....0.0-00 2 O
© | Claystone .:......... Oe2
£7 | Very stiff clay 10 10
# Clay, full of rounded black flint pebbles O 9
ee Hear GasaniGiy, wees sncsss ce secaeiececetas foaielse 22 3
Blue clay (to bottom of boring)............ 39 =O
Discussion.
Prof. Ramsay called attention to the value attaching to such
observations as those of the author on the nature of the superficial
deposits as distinct from the older rocks on which they repose.
Mr. Erneripeér observed that the presence of the Lingula deter-
mined the position of the Bognor beds in the series, though there
appeared great difficulty in fixing it stratigraphically. The com-
mingling of species exhibited in this instance, of shells hitherto
supposed to be peculiar to certain horizons, he regarded as very re-
markable.
Prof. Morris observed that the section seemed to show, not only
the order of the beds, but their manner of deposition, the whole
having formed part of a tranquil sea-bottom. He remarked on the
difficulty of separating the more recent mud deposits from the beds
of more ancient date. He pointed out the method of formation
of septaria apparently by segregation, as. they sometimes included
undisturbed parts of the beds. The number of bivalves bored by
carnivorous mollusks was remarkable, as was also the absence of
Pectunculus.
Mr. Gwyn Jrrrreys observed on the habits of Lingula, which had
been by some regarded as an annelid, and not as a mollusk. It
afforded a curious instance’ of the persistence of species, as there was
no distinction that could be established between those of the Crag
and of Silurian times. It lived at the present time between high-
and low-water mark, and the Panopea at a slightly lower level, and
probably had done so in Tertiary times.
Mr. Evans inquired whether the upper gravel, like that on the
shore of Southampton Water, contained any flint implements.
Mr. Mryer replied that he had not examined the gravels with that
view.
90 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 21,
2. Notxs on some new Crustaceans from the Lowrr Kocensz of Porrs-
moutH. By Henry Woopwarp, Esq., F.G.S., F.Z.8., of the
British Museum.
[Plate IV.]
Havine been favoured by Messrs. C. J. A. Meyer and Caleb Evans
with the opportunity of examining three new Crustaceans recently
obtained by them from the Lower Tertiary Deposits exposed during
the excavations for the “Dockyard Extension Works” in Ports-
mouth Harbour, I beg to submit the following notes thereon.
I. Family Coryvstpx. (Genus Paleocorystes, Bell.)
This family, represented at the present day by the genus Corystes
common on our own coast, and in the Chalk, Greensand, and Gault
by the genera Paleocorystes and Eucorystes, has now been discovered
in the Lower Eocene, at Portsmouth, by Mr. Caleb Evans, F.G.S.
The specimen (see Plate IV., figs. 1 a, 6), although far from per-
fect, is sufficient to indicate at once the genus to which it belongs,
namely Palcocorystes, and also that it is specifically distinct from
those occurring Jn the Cretaceous rocks, already described by Prof.
Bell and others*. The carapace measures one inch in length; but
(both its anterior and posterior borders having been injured) it
was, originally, probably nearly one-fourth of an inch longer. In
breadth it measures 10 lines. Some portion of the anterior (orbital
and suborbital) border can still be traced out; but the rostrum is
quite destroyed. The surface of the carapace is smooth and devoid
of ornamentation, save a few widely scattered and very minute
puncta ; but where the delicate cortical layer has been removed, the
carapace presents a finely granular structure. The two sigmoid
markings, observable on the carapaces of all the Corystide are also
- clearly to be seen in this example.
On the underside the branchiostegal pieces (br) are traceable,
also the basal joint (m) of one of the maxillipedes (see Plate IV.
fig. 1 6). :
I propose to name this form Palewocorystes glabra. Previously to
the discovery of this crab no species of Palwocorystes had been met
with in any bed younger than the Maestricht Chalk, where a species
named P. (Notopocorystes) Miullert has been noticed by Count von
Binkhorst, which much resembles P. glabra, save that the sigmoidal
markings seen on the latter are absent in the former species. (See
Plate IV. fig. 2.)
This is the second family of Crustaceans living at the present day,
and met with fossil in the Maestricht Chalk, which I have had the
pleasure of recording as occurring also in the Eocene of the south
of England?t.
* See Prof. Bell’s Monograph on the Fossil Crustacea of the Gault and Green-
sand, Palzontographical Society, 1862, vol. xiv. p. 11, pls. 1. & iii.
+ See British Association Reports, Norwich, 1868, on the Occurrence of Cal-
lianassa Batei in the Upper Marine Series, Hempstead, Isle of Wight, p. 75,
pl. 2. fig. 4.
1870.] WOODWARD—LOWER-EOCENE CRUSTACEA. 91
II. Family Porrunipm. (Gen. nov. Rhachiosoma.)
Amongst the pelagic Crustaceans we find numerous examples be-
longing to the Portunide, all armed with long spines on the hepatic
region, and with the lateral borders of the carapace greatly produced.
Thus the genera Matuta, Orithyia, Podophthalmus, Portunus, Lupea,
and many other forms possess long hepatic spines.
Two Eocene genera have also been described and figured by Dr.
Alphonse Milne-Edwards in his ‘ Histoire des Crustacés Podoph-
thalmaires Fossiles,’ namely, Hnoplonotus armatus, from the Num-
mulitic beds, Salcedo, and the Psammocarcinus Hericartu (Plate IV.
fig. 4), from the Sables de Beauchamp (Lower Eocene). We are
now, by Mr. Meyer’s exertions, made acquainted with two new
forms (see Plate IV. figs. 3 and 5) from the Lower Eocene of
Portsmouth, which it is proposed to place in a new genus, the
characters presented by the carapace in the specimens under con-
sideration not warranting us in referring them with certainty to any
genus of fossil Crustacea already established.
RHACHIOSOMA*, gen. Nov.
Carapace produced laterally into two more or less long and
pointed spines; latero-anterior border also furnished with spines ;
surface of carapace tuberculated.
1. RacHrosoMA BISPINOSA, sp. nov. (Plate IV. fig. 3.)
This form is remarkable for the great development of its two
lateral spines, which in length exceed half the breadth of the
carapace. In section they are nearly round, slightly recurved at
their extremities, and taper gradually to a point. The carapace
itself measures 1 inch in length and 13 inch in breadth (exclusive
of the hepatic spines, which are each 10 lines in length).
The cardiac region is separated from the branchial regions by two
undulating subcentral furrows, and bears a single tubercle upon its
centre. The gastric region is ornamented with two small subcentral
tubercles. Two prominent equidistant tubercles mark the centre-
line of the branchial region, and form, with a third on the meso-
gastric region, a prominent ridge on either side the mesial line of
the carapace, iiclined towards the rostrum at an angle of about
80°. A solitary tubercle on the hepatic region, just in front of the
base of the great hepatic spine, completes the ornamentation of the
surface of the carapace.
The latero-anterior border appears to have been armed with two
or more marginal spines; but the intense hardness of the matrix
(a fine-grained quartzite) in which the specimen is imbedded has
rendered its development unsuccessful. The posterior border of the
carapace is half an inch broad.
The surface of the carapace (where preserved) shows it to have
been very minutely and delicately punctate.
* From payis and cpa.
92 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec ik
The specimen was obtained from a mass of quartzite, and rests
enclosed in a portion of the body-chamber of a Nautilus imperialis.
2. RwacHtosoma ECHINATA, Sp. nov. (Plate IV. fig. 5.)
This handsome crustacean, which must have measured 33 inches
from tip to tip of its lateral spines, and 14 inch from the anterior
to the posterior border of its carapace, is far more robust than the
preceding species. The hepatic spines are only 3 an inch in length,
and develope a small branch spine midway upon their anterior
border, resembling in this character the hepatic spines of Psammo-
carcinus Hericartii (see Plate IV. fig. 4).
The arrangement of the tubercles agrees with that in the foregoing
species (2. bispinosa), save that around the central tubercle on the
cardiac region there are placed three very minute tubercles, whilst
two others, equally minute, mark the metacardiac region. The latero-
anterior border gives evidence of three marginal spines on either
side, all of which, however, have been broken off. The frontal
border is quite lost, although most carefully attempted to be worked
out by an experienced hand; the extreme hardness of the matrix (a
fine-grained and very hard quartzite), as in the former case,
defying development. Where the surface of the carapace has been
preserved it is finely punctate. The chelate fore-hand is preserved
on the right side, exhibiting 3 joints, and measuring about 13
inch in length.
EXPLANATION OF PLATE IV.
Fig. 1 a. Dorsal aspect of carapace of Paleocorystes glabra, H. Woodw. (nat.
size), from the Lower Eocene, Portsmouth.
Fig. 14. The same, seen from the underside: m. maxillipede ; 7. branchiostegal
piece.
From the Cabinet of Caleb Evans, Hsq., F.G.S.
Fig. 2. Paleocorystes (Notopocorystes) Miillert, Binkh. (two-thirds natural size),
from the Uppermost Chalk, Maestricht. (Copied from tab. ix. fig. 14,
Mon. des Gastéropodes et des Céphalopodes de la Craie Supérieure
de Limbourg, by J. Van den Binkhorst, 1861; figured for com-
parison with P. glabra.)
Fig. 3. Rhachiosoma bispinosa, H. Woodw. (nat. size), from the Lower Eocene,
Portsmouth.
From the Cabinet of C. J. A. Meyer, Hsq., F.G.S.
Fig. 4. Psammocarcinus Hericartii, Desmar., sp. (twice nat. size), from the Sables
de Beauchamp (Lower Eocene). (Copied from the Hist. des Crus-
tacés Podophthalmaires Fossiles, by Alph. Milne-Edwards, tome i.
pl. 10, fig. 1. Paris, 4to, 1861).
Fig. 5. Rhachiosoma echinata, H. Woodw. (nat. size), from the Lower Eocene,
Portsmouth.
From the Cabinet of C. J. A. Meyer, Esq., F.G.S.
3. On the Cuarx of the Crirrs from SrarorpD to EastBourne, SussEx.
By W. Wartaxrer, Esq., B.A. (Lond.), F.G.S.*
* This paper has been withdrawn by the author by consent of the Council.
Quart .Journ. Geol. Soc. Vol XXVIL PL IV.
GH Ford.
NEW FORMS
Mintem Bro> imp
OF BOCENE CRUSTACEA:
1870.]° | WHITAKER—SOUTH DORSET AND DEVON CHALK. 93
4.—On the Cuatx of the Sournern Part of Dorset and Devon*.
By Wirtr1am Waitaker, Ksq., B.A. (Lond.), F.G.8., of the Geological
Survey of England.
As my rambles through Dorset and Devon (in 1867-68) were made
from east to west, the same course will be followed in transcribing
my notes, a course that will also have the advantage of starting
from the point nearest to the Isle of Wight, the Chalk of which
has been described in a paper of which this may be taken as a con-
tinuation +.
At the northern side of Swanage Bay, where the rocks are almost
vertical, the Upper Greensand, consisting of green-grey sand with
layers of nodular stones, is capped by evenly bedded Chalk Marl,
made up of alternations of lighter-coloured thicker and harder beds,
with darker thinner and softer, and forming a sort of ridge-and-
furrow foreshore, as in the Isle of Wight. The Chalk Marl has a
thick grey bed at top, and seems to be about 60 feet thick. It is
succeeded by hard bedded Chalk without flints, which again is soon
succeeded by a thin layer of the Chalk-rock, hard, with the usual ir-
regular-shaped green-coated nodular lumps (chiefly at the top) and
iron-pyrites. Above this is Chalk that weathers to a rough surface,
and higher up contains flints. Further east, at the highest part of
the cliff, the Chalk is less rough, and not so full of flints as in the
Isle of Wight.
I was not able to get at the section between Ballard Hole and the
Foreland ; but enough has been already written on that partt. I
may remark, however, that two of the isolated pinnacles of Chalk
still have a little turf on the top, and so show the former continua-
ticn of the land-surface, with its smooth sloping contour, due to sub-
aérial denudation, and greatly differing from the abrupt cliff against
which the sea washes. The cliff does not cut through the highest
part of the escarpment, but seems here to be along the flank of an old
pass or gap.
In Studland Bay the junction of the Reading Beds and the Chalk
is piped; but this is hardly.enough to prove unconformity between
the two formations.
At the gap in the escarpment between Ballard and Nine-Barrow
Downs the almost vertical bedding is marked in part by distinct
even and parallel lines in the turf, caused by difference of growth
on harder and softer beds.
A small pit on the flank of the escarpment about a mile and a
half eastward of Corfe Castle shows a northerly dip of about 60° in
the following beds :—
* The district referred to is represented in Sheets, 16, 17, & 22 of the Map
of the Geological Survey of England.
ft Quart. Journ. Geol. Soc. vol. xxi. p. 400.
¢ Rev. W. D. Conybeare, ‘ Outlines of the Geology of England and Wales,’
p- 110 (1822); Rev. W. B. Clarke, Mag. Nat. Hist. vol. x. pp. 414, 461 (1837) ;
Dr. J. Mitchell, ibzd., p. 587; T. Webster in Englefield’s ‘History of the Isle of
Wight.’
94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 21,
Chalk, with flints in the top part; at the bottom a thin fissile greenish layer
(which also occurs on the coast eastwards). ;
Chalk-rock ; a layer of hard green nodules, the upper surface better marked
than the lower.
Chalk without flints.
In a larger pit, at the kiln above Rollington, on the northern side
of the range, and therefore in the higher part of the Chalk, there
are but few flints.
' The step-like outline of the top of the hills from Corfe Castle to
Nine-Barrow Down has been noticed elsewhere *. Westward of the
former place the range again rises by steps in a like manner, and is
partly breached at the western end of Knowl Hill. Here there is a
pit in Chalk with few flints, at the northern foot of the hill, whilst
further south, and therefore lower down stratigraphically, another
pit shows Chalk with layers of flints, and with a sort of slickenside-
surfaces at right angles to the bedding. Still further south, the road-
cutting up the slope southwards is in Chalk with flints; but at the
top of the rather low hill the flints seem to end, and as the road turns
down again eastward the hard cream-coloured nodular Chalk-rock is
shown, and below it Chalk without flints.
From this slight gap in the escarpment a longitudinal combe runs
westward as far as Screech Barrow, making two ridges. Screech
Barrow itself is a conical Tertiary hill, close to and rising above the
chalk-escarpment.
Signs of the Chalk-rock were again seen on the newly cut road
above West Tyneham.
There are many small pits on the flank of the escarpment in the
so-called Isle of Purbeck, showing Chalk Marl and Lower Chalk,
but not high enough to touch the Chalk-rock. The Chalk is through-
out rather hard.
Flower’s Barrow, on the top of the ridge where it again meets the
sea, is one of those instructive gauges of the loss of land by the sea
that are often given us by the old earthworks. Nearly half of the
entrenchment has been carried away, and the high cliff now cuts
through its middle part. Here the top part of the Upper Greensand
stands out, from its hardness. I could not see the Chalk-rock along
the top of the cliff, nor could I get near enough to the foot in a
boat ; but a bluish-grey clayey bed. some feet thick, could be made
out at the top part of the Chalk Marl, as in the eastern coast-section.
At the headland on the western side of Worbarrow Bay there is a
natural arch at the foot of the cliff, through which small boats
can go.
In Mewps Bay the following succession of beds may be seen along
the shore :-—
Chalk with flints, running out to sea as a ledge, with a hollow and
oe La cave cut in the cliff.
~~ | Chalk without flints (?), about 15 feet.
* ©On Subaérial Denudation and on Cliffs and Escarpments in the Chalk and
the Lower Tertiary Beds.’ Reprinted, with corrections &ec., from the Geol.
Mag. vol. iy.
1870. | WHITAKER—SOUTH DORSET AND DEVON CHALK. 95
Lower f Chalk-rock nodules, at a ledge running out into the shingle-beach.
Chalk. Chalk without flints.
Chalk Marl, more or less hard.
Upper Greensand.—Green- -grey and partly hard. Along the top of the cliff
the top part of this is caleareous, and passes up into the Chalk Marl.
At Lulworth Cove the fallen state of the cliff hid much of the
accessible part of the section ; but the grey soft layer at or near the
top of the Chalk Marl was to be seen.
In Man-of-war Cove I could not see the Chalk-rock at the eastern
part, where the junction of the Upper and Lower Chalk seems to be
much confused. Westward, however, the nodules of the rock are to
be seen up to a height of 5 feet above the beach, when they are cut
off by Chalk, again with confused bedding, soon succeeded by Chalk
with flints, also somewhat confused. Still further west the nodules
again occur, and the Upper Chalk is less than 80 feet from the Upper
Greensand, the bedding of which latter and of the Chalk Marl is
reversed, being at an angle of about 70° 8.8.W. instead of north-
wards. The Chalk Marl seems at one part to be 45 feet thick. It
has the usual darker clayey bed at top, whilst the bottom 2 feet or
more contains dark grains, small brown nodules, and grains of
quartz. The top part of the Upper Greensand is hard from its large
irregular-shaped nodules of chert ; and the topmost 2 feet or more is
sometimes a buff cherty sandstone.
At the eastern end of Durdle Cove the dip of the Chalk Marl and
the Upper Greensand is still reversed southwards, at an angle of 80°.
The former, with its grey soft layer near the top, is succeeded by
Chalk with a few flints ; and, indeed, there is one layer of flints less
than 20 feet from the Upper Greensand, and therefore in the Chalk
Marl, which, however, is here not clearly separable from the Chalk
above. A little westward the Chalk with flints comes on; and the
bedding is confused at the bottom of the cliff, as in Man-of-war
Cove. On turning the corner, into the deeper part of the Cove, a
cream-coloured and partly greenish layer of nodules (like those of the
Chalk-rock) may be seen. Beyond this the frequent layers of flint
show a southerly or reversed dip of about 65°, soon changing to a
higher angle, and afterwards to a curved dip in the other direction,
30° at the top, and 60° or more at the bottom of the cliff, as shown
ro tio le
Fig. 1.—Section of the Chalk with flints. Eastern side of Durdle
Cove.
—$ —$
—_ ee aA Ge AY
F PUGET
pape
“ ee, Ty Sf Chi / fey My. {|
i CE \
Vy, f q | rity", NN
f Mil Mh \ AN
; : \\ \ \
ed SME
y ——
a. Beach-line. b. Fallen earth.
ec. Chalk with Flints. d, Nodule-layer.
96 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 21,
On the western side of the Cove also the bedding is rather curved.
At White Nore * the lower beds are hidden by an undercliff on
the west, where there is but a very slight easterly dip ; but the general
section is as follows :—
Irregular capping of flints and clay-with-flints all along the high cliff.
Chalk with many layers of flints, and some cream-coloured nodular layers ;
one near the bottom of the first cliff is 14 foot thick; another, 2 feet below
at one part, joins it in a distance of 20 or 30 yards.
Chalk without flints, or with very few flints, in part weathering roughly (in
layers), as certain beds in the Dover and Beachy Head sections.
Chalk Marl, with flint-layers. and with a soft grey layer some 40 or 50 feet
from the bottom, which, from its weathering away easily, has given rise to
a slight ledge. ’
Upper Greensand.—The junction the same as at Durdle Cove &c.
I could not well make out the junction of the Upper and Lower
Chalk, in the midst of the cliff; it seemed to be faulted and nearly
vertical.
From hence westward the Chalk leaves the coast for many miles,
though it sometimes comes near the sea. ;
At a spring-head above Ringstead a small pit shows a vertical
junction of Upper Greensand and Chalk Marl. There are a few
flints in the latter ; and its bottom bed, with dark grains and quartz
grains, is thicker than in the coast-sections above noticed. The same
junction is again laid open by a road-section, about half a mile N.W.
of Sutton Pointz. ;
From Upway westward to Portisham the Chalk is bounded by a
fault, according to the Geological Survey Map, and consequently its
bottom part does not crop out to the surface.
The next junction with the Upper Greensand that I saw is at a
farm called “‘ Higher Combe,” about five miles east of Bridport,
where the very bottom of the Chalk Marl is in the form of hard
lumps, with some hard nodules (greenish outside), and fossils in
plenty.
funea tion Hill +, N.E. of Bridport, the Upper Greensand forms
rocky ledges at the base of the Chalk, the highest being of a more or
less calcareous grit, and the next of irregularly weathered (? calea-
reous) sandstone, with dark grains and full of fossils. Between these
is green-grey sand, full of stony nodules in the higher part, and,
indeed passing up into the stone above. The grey rocks, clad with
lichen, small ferns, and ivy, are very pretty. On turning from the
side of the hill facing Powerstock, round the sharp ridge formed by
the Upper Greensand, to the side facing seaward, the upper rock-bed
is seen to crop out evenly along the flank, and to dip slightly south-
ward ; whilst above it is the bottom Chalk Marl, with dark grains and
quartz-grains ; 2 feet up the grains get fewer, and they are lost at
about 4 feet.
Westward from Bridport the Chalk does not occur near the coast,
* So spelt on the Ordnance Map. Should it not be “‘ White Nose”? a fit name
for a chalk headland. ,
7 Just in Sheet 18 of the Geological-Survey Map.
wy
1870. ] WHITAKER—SOUTH DORSET AND DEVON CHALK. 97
until we pass the border of Dorsetshire, just beyond Lyme Regis, and
enter Devonshire, where the high cliffs are broken by the great range
of landslips that add so much to their beauty. ‘The sections here
have been described by Sir H. De la Beche *; and from his account
of the Chalk seen near Lyme it appears that the lower, or flintless,
division is thin, having a thickness indeed of not more than 40 feet,
whilst the lowermost 50 feet of the Upper Chalk contains fewer flints
than the overlying part, in which they are frequent. I cannot un-
derstand, though, how so great a thickness as 20 feet is given by
him to the Chalk with quartz-grains, unless, as seems likely, the
whole of the Chalk Marl is therein included.
In the Chalk with flints at Pinhay +} &c. there are brown hard
nodular layers, weathering to a rough surface, as at White Nore, east
of Weymouth. In the undercliff fallen masses show the junction of
the Chalk and the Greensand, the bottom of the former consisting of a
hard buff nodular bed, with dark grains and quartz-grains, from 2
to 3 feet thick, above which, for from 2 to 4 feet, the Chalk has irre-
gular masses of the same brown nodular character, and also the
distinctive grains. Here, indeed, it is often hard to mark the junc-
tion; the Chalk gets nodular, darker, and harder, until it seems
almost one mass with the Greensand.
Near the cliff-top just east of Charton, the junction may be seen
in place, the same two beds occurring, and the upper of them passing
up into white chalk with hard brownish nodular lumps, which (8
or 10 feet above the greensand) form a projecting bed about 13
foot thick. Some of the quartz-grains here are larger than those in
the country to the east.
At the western end of the Dowland’s landslip the bottom six
feet of the chalk are hard, quartz-grains occur therein, and the
lower part is slightly darker and compact.
At the mouth of the Axe the bed with quartz-grains is about
three feet thick and contains fossils.
The section near Beer has also been described by Sir H. De La
Beche; but something may be added to his account. The chalk-
with-flints of White Cliff contains hard buff nodular layers (as else-
where), and its bottom part has fewer flints than the rest. The
chalk without flints also contains hard nodular layers, and is of
comparatively small thickness, perhaps thirty feet ; the lowermost
three feet or so are the same as to the east.
Westward of Beer Head the bold cliffs, here separated from the
sea by a fine undercliff, give a most interesting section, part of
which shows a thinning-out of the Lower Chalk, and consequently
the direct superposition of Upper Chalk on Upper Greensand—an
occurrence which I believe has not been before noticed in this country.
This junction is inaccessible, and can be seen only from below, and
then, from the roughness of the cliff, not with the greatest ease.
In fig. 2 it has been thrown into the form of a diagram, as it would
* Trans. Geol. Soc. ser. 2, vol. ii. p. 110, and “ Report on the Geology of
Cornwatl, Devon, and West Somerset,” p. 237.
+ Pinney on the Ordnance Map.
VOL, XXVII.—PART I. zee
Me
st of Beer Heac
a
0
er part of the Cliff we
——DNagram of a portion of the upp
9
PROCEEDINGS OF THE GEOLOGICAL SOCTETY. | Dec2ae
5
6
hard
calcareous grit and sand-
stone.
St
POS
= a4 8 5
7
eee
6. Upper Greensand :
with green grains, quartz-grains, and
lar lumps.
eous bed, of lighter colour and with fewer grains.
4
areous bed,
nodu
Calcar
| =
(4. Cale
{s
7
po =
Chalk
Marl?
. Nodular bed (Chalk rock 7).
Chalk without flints.
1. Chalk with flints.
9
3.
Chalk. }
be difficult to draw the actual cliff with
its succession of irregular projections.
The junction of the Chalk without
flints and the Greensand may be seen
amongst the fallen masses west of the
landslip (of 1790). In the cliff the no-
dular Lower Chalk is underlain by, and
passes into, a calcareous bed (4 of fig. 2)
full of green grains and quartz-grains,
with lghter-coloured harder nodular
lumps and small hard brown nodules,
about five feet thick ; below this is a hard
brown and greenish nodular layer, also
with quartz-grains, forming the top of
the succeeding bed (5 of fig. 2), which
is like that above (but whiter and with
fewer grains), and five feet thick; it is
underlain by another nodular layer that
forms the top of a calcareous grit
(Greensand). The two beds, 4 and 5,
seem to thin out westward as in the
figure, the higher one going the further.
The opening of the gallery of an old
quarry in the high cliff above the western
end of the great landslip is in what I
take to be the “Beer stone.” As the
beds worked are just above the Chalk
Marl, it follows that they are simply
Lower Chalk; and this conclusion as to
the position of the Beer stone is strength-
ened by an examination of the great
quarry inland, where the stone is still
worked.
This quarry is about three quarters of
a mile westward of the village of Beer ;
and at the time of my visit the part on
the northern side of the road gave the
section below, with a dip of 4° E.
Chalk with flints ............... 30 or 40 feet.
(a. Vhickly bedded, massive, with
arough layer on top(mostly
forming a hard even cap)... 15ormore.
} 6, Massive, more crystalline bed
4 (“‘freestome?”) /........ about 10
e. More splintering, and with
Chalk without Flints.
\ [UII REE eagle oe oe about 8
~~
? Chalk Marl. Bottom part with a _
few quartz-grains and black grains.
a, b, §c. are all parts of one mass,
1870. | WHITAKER—SOUTH DORSET AND DEVON CHALK. 99
without marked divisions; and the Beer stone must take its place
therefore simply as Lower Chalk.
To return to the cliffs. Near Branscombe there is white hard
Lower Chalk over the cream-coloured sandstone of the Greensand ;
but sometimes a flint-layer occurs little more than a foot above the
latter. At the highest part of the cliff the section is :—
Irregular pipy deposit of flints.
Chalk with fints.
Chalk without flints, but with hard cream-coloured nodules, 30 or 40 feet.
Sandstone (Greensand).
A little westward there is a layer of flints a few feet above the
Greensand, to which also the Chalk with flints is nearer. Still further
westward, where the cliff again rises, a thick continuous deposit of
flints caps the Chalk, and there are signs of the bed with quartz-
‘grains at the bottom of the latter. Then a part of the section
(fig. 3) shows flint-layers, some of which end abruptly—and some
nodular layers not parallel with the former, but cutting through
them.
Fig. 3.—Section of part of the top of the Cliff west of
Branscombe Mouth.
y =”
a) pte
y
y
. Flint-gravel.
. Chalk with many layers of flint.
3. Nodular layers.
: ae with a few layers of flint and of marl, and a layer of nodules.
. Talus.
At the small outlier on the hill west of Weston Mouth, the most
westerly patch of chalk shown on the Geological Survey Map,
hardly any thing can be seen, from the great surface-deposit of flints;
but at the next cliff beyond, just east of Saleombe Mouth, there is
again a little chalk, which I believe to be the most westerly mass of
that rock now existing in England.
The above notes must be taken as merely a record of a few facts
HZ
toe
Ou ee
100 PROCEEDINGS OF THE GEOLOGICAL soctETy. [ Dec. 21, 1870.
observed in a summer ramble, from which, however, the following
general conclusions may be rawn.
(1) That along the South Coast of England the Chalk Marl thins
westward from the Isle of Wight, where it is in good force, and its
bottom part becomes marked, in that direction, by the presence of
quartz-grains, mostly very small, but sometimes as large as a pea,
showing perhaps signs of a less deep-sea character than usual in
the deposit. This bottom bed is the most constant part westward,
where, indeed, it seems sometimes to be all that represents the Chalk
Marl.
(2) That along the South Coast the Lower Chalk, of no very
great thickness in the Isle of Wight (about 200 feet perhaps), thins
westward until in Devonshire it is but 30 feet thick, and occasion-
ally less.
(3) The consequent nearness of the Upper Chalk (with flints) to
the Greensand helps to explain the occurrence of the great deposits
of flints on the hills of the latter im Devonshire.
Discussion.
Mr. Erreripce pointed out the resemblance between the series
described by the author and that of the Chalk of Antrim. He
thought it probable that the Cretaceous beds had originally ex-
tended over the whole of Western England. He called attention
to the Blackdown beds, which had been regarded as Upper Green-
sand, but certainly were not so, though probably Cretaceous, as well
worthy of examination.
Mr. Hutt hoped that some Fellows of the Geological Society
would extend their examination of the Chalk into Ireland, and visit
the Antrim district. It was the case there that the Chalk with flints
rested immediately on the Upper Greensand, though there was an
intermediate band known as the Mulatto-bed, which might possibly
represent the Chalk-rock.
Prof. Morris thought the paper afforded evidence in favour of the
Chalk having been deposited in a sinking area, and during the pro-
cess various alterations in the conditions took place.
Mr. D. Forszs inquired as to the character of the nodules men-
tioned, and whether they were siliceous or not.
Mr. Meyer mentioned that near Branscombe there occurred a band
within 8 feet of the Red Marl, containing fossils apparently the same
as those of Blackdown.
Mr. Wuitaxer had purposely avoided characterizing the greater
part of the Greensand-beds as either Upper or Lower. He thought
the cherty beds of the west were stratigraphically higher than
those of the Isle of Wight. The nodules inquired about were not
siliceous, though probably containing some silica, but were rather
phosphatic.
Jan. 11,1871.] samrusoN—BANFFSHIRE MEraMoRPHiC Rocks. 101
January 11, 1871.
William Salter, Esq., of Maldon, Victoria, Australia, was elected
a Fellow of the Society.
The following communications. were read :—
1. On the OxpER Metamorpnic Rocks and Granite of BaNFFSHIRE.
By T. F. Jamruson, Esq., F.G.S.
Contents.
Introductory.
The three divisions of the strata.
1. The lower division, or Gneiss and Quartz-rock.
2. The middle division, or Slates.
3. The upper division, or Upper Quartz-rock.
The Granite—its origin. i
Theory of the derivation of the sedimentary strata and of their present strike.
InTRODUCTORY.
Tue information we have regarding the geology of Banffshire is
chiefly to be found in Dr. MacCulloch’s map of Scotland, a memoir
by R. J. Cunningham in the Transactions of the Highland Society,
2nd ser. vol. vii. p. 447, and a paper by Professor Harkness in the
Quart. Journ. of the Geol. Soc. for 1862, vol. xvii. p. 331.
Mr. Cunningham’s memoir deals with the structure of the whole
county, and is accompanied by a map and some sections, while the
paper of Professor Harkness describes the section of the rocks ex-
posed along the coast. I have carefully examined the whole of the
section described by Professor Harkness, and also the coast eastward
as far as Fraserburgh ; but being unable to satisfy myself as to the
true succession of all the various beds which are there exposed, I
betook myself to the interior of the country; and from an examina-
tion of the district lying between the Spey and the Deveron, I was
enabled to arrive at clearer views regarding the relation of the
various strata to one another, and have constructed a section (fig. 1)
extending from near the village of Rothes, on the river Spey, in a
south-easterly direction by Mortlach, and the Old Castle of Auchen-
down, for a distance of about twelve miles, which shows the succes-
sion of the beds very distinctly.
THE THREE DIVISIONS OF THE STRATA.
At the bottom we have a great thickness of arenaceous beds, which
rise up at the western end of the section, beside the river Spey, and
are more or less altered by metamorphic action into quartz-rock, gneiss,
and mica-schist (fig. 1,a). The base of this series is not exposed, and
it seems to extend across the Spey for some distance into Morayshire.
In tracing the section eastward, we find these lowermost beds dis-
appearing underneath a series of fine-grained argillaceous beds or
clay slate (fig. 1,), varying in colour from green to a very dark, almost
102
Fig. 1.—Seetion from the Spey to the Deveron, a distance of 12 miles.
sl
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¢e. The upper quartz-rock.
1. Limestone.
b. The middle division, or slates.
a, The lower gneiss and quartz-rock.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 11,
blackish hue. In the midst of this mass
of clay-slate there is a bed of limestone
(fig. 17); and both the limestone and
the slate beside it often contain a large
proportion of magnesia, and the vary-
ing metamorphism of these beds has
in some localities given rise to masses of
serpentine and talcose slate. This slaty
series is covered by a second or upper
group of arenaceous strata (fig. 1c),
often assuming the character of quartz-
rock of a very pure white colour, form- ©
ing the top of many of the hills of this
district. Although in many places this
upper quartz-rock is much worn away,
yet in some of the mountains in the
higher parts of the county it attains a
great thickness, and forms the upper-
most bed of the old metamorphic rocks
exposed in this region.
We see therefore that the arrange-
ment and succession of the metamor-
phic strata here are very similar to
what we find in Bute and Argyleshire
(see Quart. Journ. of Geol. Soc. 1860,
vol. xvii. p. 183), namely a mass of
clay-slate enclosed like a sandwich be-
tween two great masses of arenaceous
beds. The rocks of Banffshire, in fact,
seem to belong to the same formation
as those of Bute. That is to say, they
form the north-eastern extension of
those beds which range through the
central Highlands of Scotland, from
the Moray Firth to the Firth of Clyde.
Jn mineral quality and state of meta-
morphism the resemblance is very
close.
1. The Lower Division, or Gneiss and
Quartz-rock.—The passage from the
lower quartz-rock upwards into the
slates may be clearly seen along the
course of a small stream, locally
known as the Burn of Mulben, on the
east side of the Spey, which is tra-
versed by the line of railway from
Keith to Elgin. Near the mouth of
the stream, where it falls mto the
Spey, the mineral quality of the rock
is, when freshly broken, white and
1871.] | JAMIESON—BANFFSHIRE METAMORPHIC ROCKS, 103
quartzose, almost a pure quartz-rock, with ferruginous stains along
the joints and planes of division. In Mac Culloch’s map it is by
some mistake coloured as part of the Old Red Sandstone, its
arenaceous character having probably in some measure led to
the error. As we proceed up the course of the stream the rock
is seen to lie in gentle undulations dipping south-east at a low
angle, the quality still much the same, but rather more mica-
ceous—heing a fine-grained micaceous quartz-rock, or quartzose
mica-slate. Near its junction with the slate the rock becomes more
micaceous—a ferruginous-stained micaceous grit, alternating with
seams of mica-slate, often thin-bedded and well laminated lying in
regular order and dipping south-east, at an angle of 30° or 35°.
The colour now becomes greener and the lamination more distinct ;
and the passage upwards into the base of the overlying mass of
slate is thus accomplished, there being thin seams of grit interbedded
with the slate where it commences. The slate is here of a dull
greenish colour, and is well exposed along the railway on to Mulben
station, dipping south-east at from 30° to 40°. The mineral charac-
ter of the group of rocks lying beneath the slate series may also be
well studied along the western flank of Ben Aigan, where there are
some deep gullies cutting far into the hill. ‘The whole of this side
of the mountain from top to bottom consists of these rocks, indica-
ting a thickness of about 1200 or 1400 feet; and as they seem to
extend across the Spey for some distance westward, the depth is pro-
bably very great. In such a mass of sedimentary strata there must
of course be a considerable variety in the quality; and although the
general character is quartzose, yet seams and beds of a softer and
more slaty nature may here and there be met with. At one place I
found the strata so rotten that considerable masses were reduced to
the consistency of mud. The crushing, squeezing, and twisting to
which the beds have been exposed have probably had something to
do with this; and the occurrence of such rotten beds here and there
in a mountain must greatly facilitate the operation of those forces
which carve out valleys and have removed such immense quantities
of rock from the surface in many places. The rapidity with which
the waste occasionally goes on may be seen in a deep gully or trench
in the west flank of Ben Aigan, which seems to have been excavated
by the action of a petty stream of water, so insignificant that at
some seasons of the year it is almost quite dry.
Similar masses of rotten rock, approaching the consistency of soft
sandy mud, occur near the top of the Glenmarkie ridge to the east
of Auchendown Castle, in the upper quartz, although part of the
strata in the immediate neighbourhood is a hard-grained white quartz-
rock, or metamorphic grit. It is interesting to examine this mould-
ering bank of rusty brown sand and mud, containing some seams
of disintegrated slate, where we see the rock reduced to something
like what we may suppose to have been the original condition of the
bed when it lay at the bottom of the ancient sea.
In some places the lower quartz-rock is much impregnated with
oxide of iron ; and at Arndilly, on the west base of Ben Aigan, an at-
104 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 11,
tempt was made to work a small vein of ironstone which occurs there.
On the top of the hill the rock is of purer quality ; and along the
eastern slope it is covered by the clay-slate, which, however, seems
to have its stratification more disturbed than at Mulben, and the
junction is not so well exposed.
If the quartzose gneiss on the west side of the Spey comes out
beneath the basement beds of Ben Aigan, as seems probable from
the disposition of the strata, it would show that the thickness of the
group of rocks lying beneath the slate is very considerable. The
quartz=rock of Cullen lies on the line of strike of the Ben Aigan
quartz, and is probably the northern extension of the same strata.
2. The Middle Division, or Slates.—With regard to the slate, the
lower portion, as I have already mentioned, is well exposed to view
along the line of railway at Mulben, and on the coast between
Gamrie Head and Macduff there is a fine section. The limestone is
exposed in a great many places along the river Dullan at Mortlach,
the Loch of Drummuir, Auchendown Castle, &e. Its thickness varies
a good deal in different places; and in the coast-section between
Gamrie and Macduff no limestone occurs, so that it would seem
occasionally to thin out altogether.
The thickness of the slate lying between it and the upper quartz-
rock I estimated as about 500 feet in some places; and probably
there is as much beneath it, which would make a total of 1000 feet
for the mass of slates. But the thickness of the slate itself seems
to vary a good deal, and to increase towards the coast. It probably
consists of the finer sediment accumulated in deep still water, and
would be thickest in the troughs of the old sea-bottom. We
should therefore expect to find it thickening in certain directions.
So far as I can judge, the thickness of the slate in this region seems
to increase towards the trough of the Moray Firth. The arenaceous
beds, which we may suppose to have been deposited in water that
was shallower or more traversed by currents, seem to thicken, or bear
a greater proportion to the slates, as we go towards the interior of
the country, as, for example, in the region of Braemar and Glentilt,
where the quartz-rock is much developed and of great purity.
3. The Upper Division, or Upper Quartz-rock.—The meeting of the
slate with the upper quartz-rock may be seen in some of the gullies that
rut the side of the hill which forms the eastern bank of the river
Dullan, in the neighbourhood of a place known as the Giant’s Chair,
a little way above the village of Mortlach. This Giant’s Chair is an
old pot-hole worn by the former action of the stream in the lime-
stone which here forms the bed of the river. The top of the ridge
which divides the Dullan from the Fiddich consists of the upper
quartz, and so likewise does the top of that which separates the
Fiddich from the Deveron. In the latter ridge, to the east of the
old castle of Auchendown, the slate may be seen forming the base
of the Glenmarkie Hill, and has been quarried for roofing purposes
bere and there along its western slope; but the top of the ridge is
of quartz. The slate may also be seen passing underneath the upper
quartz-rock, on the eastern bank of the river Fiddich, opposite Bal-
1871.] JAMIESON—BANFFSHIRE METAMOKPHIC ROCKS. 105
venie Castle, close by the edge of the stream. Here the slate
troughs the quartz in a synelinal fold, which is much more abrupt at
one side than it is at the other; for as we walk along the river from
north-west to south-east, we find the slate disappearing under the
quartz at an angle of from 20° to 25°, and emerging again to the
south-eastward almost vertically. The quartz-rock is here much
crushed and disintegrated, as if by the nip it had got in the sharp
curve of the synclinal fold.
Tuer GRANITE—1TS ORIGIN.
The granite of this region, I am inclined to think, has resulted
from the fusion and recrystallization of the arenaceous beds. It is
evident that the granite has originated after the deposition of these
old sedimentary strata, because they are everywhere penetrated by
its veins and injected masses, as may be well seen in the district
around Lower Craigellachie. The granite, however, does not de-
range the strike of the beds to the degree that such a mass of
foreign material should have done had it been erupted in an igne-
ous condition, or foreed up in any other conceivable way. I would
rather suppose that the heat from the interior of the earth gra-
dually approached the base of these sedimentary beds and, by heat-
ing, caused them to expand and thereby become wrinkled into
huge folds, as a necessary consequence of a great mass of swollen
matter having to find room in the space occupied by the same
matter when in a cold and contracted state. The portions most
liable to be fused would be softened and dissolved in situ, and be
injected with enormous force, in consequence of the pressure, into
all the openings and crevices around them. Crystallization would
then take place as the whole very slowly cooled. In some such
way, I imagine, the granite of this region has been formed out of
the lower arenaceous and silty beds, and the greenstone of the
Portsoy district out of the more argillaceous strata. The heat, as
well as the watery vapour under such immense pressure, would pro-
bably penetrate further into the arenaceous beds than into the
closer-grained clays. These views are confirmed by finding the
granite occupying the room of what should have been gneiss or
quartz-rock and the greenstone replacing the argillaceous beds.
The serpentine of this region, as I have before mentioned, seems
to have resulted from the metamorphism of beds containing much
magnesia. In some places around Lower Craigellachie and the
southern base of Ben Aigan, the gneiss is plentifully streaked with
granite, as if partial fusion had just begun. These portions are
found along the circumference of the great mass of granite, and
seem to me to represent the gradual passage of arenaceous or silty
strata by way of gneiss into granite. And here I may mention that
the gneiss and quartz-rock of this region, even where most si-
liceous, always contains a proportion of felspar. The softening and
fusion, as it progressed, would advance more rapidly along certain
lines where the mineral matter was of such a nature as to yield most
readily to the influence of the forces acting upon it.
106 PROCEEDINGS OF THE GHOLOGICAL socrpTy. — {Jan. LI,
As examples that may be easily examined, I may cite a section on
the Dufftown Railway, at the Popine meal-. and saw-mill, near
Lower Craigellachie, also the rock at Craigellachie Bridge, and
along the side of the Fiddich from Craigellachie Station to near
Kininyie Castle. The rock of the hill called Upper Craigellachie
near Aviemore, is also of a similar nature, so that in many places I
should be at a loss to say whether the granite or the gneiss prevails.
Along the Fiddich, from Craigellachie Station to near Kininvie
Castle, the rock exposed in the railway-cuttings is a hard quartz, so
full of veins that one is occasionally in doubt whether to pronounce
it a stratified rock or a granite. In many places, where the aggre-
gation of the mineral particles is granitic (rather small-grained and
reddish), traces of the undulating bedding may be observed ; in short,
the rock seems to me to consist of the beds of lower quartz-rock
merging into granite—that is to say, incipient granite, a stratified
rock far gone on its way to granite.
In some places, near Craigellachie, there is a good deal of
greenish matter in the rock, as if it had consisted of alternations of
talcose schist or grit and quartz-rock, such as occur near the base
of the slate on the Mulben stream, and also near the Giant’s Chair,
where the upper beds of slate meet the overlying quartz-rock. I
observed that the small granite veins occasionally form alternating
laminee in the rock, and reddish streaks parallel to the bedding, the
greenish matter segregating into irregular branching plates.
The hill called Little Conval, near Dufftown, is of granite, which
at its south-eastern base I found to be large-grained and composed
of red felspar and whitish quartz, with little or no mica; but higher
up the rock becomes finer-grained, and at the top consists of a
small-grained mixture of red felspar and quartz, much resembling
some varieties of quartzose gneiss, such as that at Red Hythe
Point, as if the metamorphism decreased in intensity as it passed
upwards. The felspar, however, is redder than is usual in gneiss,
and seems to bear a larger proportion to the quartz. There are
the remains of an old stone rampart or enclosure round the crest
of this hill.
THEORY OF THE DERIVATION OF THE SEDIMENTARY STRATA AND OF
THEIR PRESENT STRIKE.
The general texture of the materials of which the gneiss, quartz-
rock, and clay-slate are composed is fine-grained, and I observed no
beds of conglomerate or large pebbles. ‘The nearest approach to these
which I saw was in the coast-section between Gamrie Head and
Melrose, near a place called the Grey Mare’s Point, where the anti-
clinal fold occurs that is shown in Prof. Harkness’s section. Here
I observed a seam composed of water-worn pebbles of white quartz,
some of which were two inches in length. This is near the base of
the slate, and is the nearest approach to a conglomerate that I
have observed. But in general there is nothing larger-grained
than what, in its original condition, would have been a coarse sand.
It is a curious circumstance that such a thick mass of sediment
—
13712] JAMIESON——BANFFSHIRE METAMORPHIC ROCKS. 107
should have been accumulated showing so little variety in character,
and without the occurrence of any large boulders or beds of conglo-
merate. Perhaps it may be explained by supposing it to have been
accumulated in the depths of the sea, off the mouth of a great river
like the Amazon, which may have been continually pouring in se-
diment, but with a current not sufficient to carry large pebbles.
The slate, or fine argillaceous sediment, between the two great
masses of arenaceous strata may be accounted for by a subsidence of
the area of deposit into deeper and stiller water, where little except
the finer sediment would be floated.
The Red (Cambrian) Sandstone and Conglomerate of the North-
west Highlands, which stretches for a hundred miles from §8.W.
to N.E., with a comparatively narrow breadth in the opposite di-
rection, looks as if it had been accumulated along a shore-line which
was probably the coast of an ancient continent of the Laurentian
gneiss. This Cambrian Sandstone is overlapped on its eastern
border by the Lower Silurian schists and quartz-rocks of the High-
lands, which we may therefore suppose to have been accumulated
at a somewhat later period, but which, in all likelihood, consist of
the sediment poured into the sea by the rivers draining the same
Laurentian region to the north-west. After a great thickness of
sediment had been accumulated, a glow of heat from beneath seems
to have approached it, and by the expansion thereby occasioned
wrinkled the mass into huge folds running from 8.W. to N.EK. The
reason why the wrinkles run in that direction, I imagine, must be
that expansion in the transverse direction was more difficult, owing
perhaps to the opposing mass of the Cambrian and Laurentian
land preventing extension towards the north-west side.
Discussion.
Prof. Ramsay observed that the general section wonderfully corre-
sponded with that given many years ago by Sir Roderick Murchison
of the Silurian and Laurentian rocks at Cape Wrath, and it seemed
to him that the large views originally propounded by Sir Roderick
were confirmed by the author. He was glad that the metamorphic
origin of granite was supported by Mr. Jamieson, as he had held
that view for many years; and he was pleased to find that opinions
which had formerly met with so many opponents were constantly
gaining acceptance. The fusion of these sedimentary rocks by meta-
morphic action was not identical with the fusion of lava; but their
fluidity might be the same; and if that were the case, there could
be no difficulty in accepting the possibility of the injection of such
fused rocks into crevices and fissures. The crumpling of the beds,
however, was due to more extensive causes than those contemplated
by the author. The proportion of igneous rock injected into con-
torted rocks, like those of North Wales, was comparatively small,
and the crumpling could hardly be due to mere local causes.
Prof. Anstrp referred to what he had observed in the north-west
part of Corsica, where about 40 feet of granite was distinctly inter-
108 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Jan. 11,
stratified between perfectly unmetamorphosed beds of sandstone and
limestone, without any alteration at the points of contact, such as
would be produced by an igneous rock. He algo cited the crumpled
strata in the Maritime Alps, in which the granites were parallel with
the other beds, and seemed to form part of them.
Mr. Carruruers mentioned that the late Prof. Fleming, twenty
years ago, had taught the same doctrine as to the nature of granite
as that held by the last speakers. He also stated that similar views
would be found expressed in Headrick’s ‘ Mineralogy of Arran.’
Mr. Davip Fores agreed that the crumpling of the strata was
not due to the intrusion of any eruptive rock. He completely dis-
agreed with Prof. Ramsay and the author as to the origin of granite,
and maintained that, in the sedimentary rocks traversed by the gra-
nite, the requisite ingredients for the formation of granite did not
exist. The proportion of felspar in quartzose rocks was infinitesimally
small, as compared with that entering into the composition of granite.
He could not accept the notion of the heat from the interior approach-
ing gradually to some portion of the surface.
Prof. Ramsay, in reply to Mr. Forbes, maintained that some of the
slaty rocks of Wales, by extreme metamorphism, would pass into
some kinds of granite. As to the conditions of metamorphism of the
rocks, this process must have gone on at a time when these older
rocks were overlain by a great thickness of more recent beds which
have since been removed by denudation.
2. On the connexion of Votcanic Action with Cuanexs of Lrvut.
By Joszrn Joun Murruy, Hsq., F.G.8.
[ Abstract. |
Tx purpose of this paper was to show that “ volcanic action is not
the cause, but the effect, of secular changes of level; and secular
changes of level are due to the subsidence of the surface of the
interior, as the interior contracts in cooling.” Change of level is a
differential action, and consequently cannot be due to the cooling of
a sphere by radiation into space. Volcanic action cannot be due to
a spontaneous outburst of the expansive force of the earth’s internal
heat ; for this could not burst through a crust once formed by cool-
ing. Changes of level and volcanic action were explained as fol-
lows :—The interior of the earth is constantly cooling, and as it
cools must contract; but the cold surface-strata cannot contract
with it; and as their weight keeps them in contact with the core,
they are compelled to form ridges like those on the skin of an apple
which shrinks in drying. When such a ridge rises into an arch,
the hot matter below rises and fills the arch, forming the igneous
core of amountain-chain. Volcanoes are formed when in these fold-
ings the surface is broken through, so as to liberate the expansive
force of the internal heat. Darwin has shown, in his work on Vol-
canic Islands, that voleanoes are formed only in regions which are
1871.| DE ORUEBA—GEOLOGY OF MALAGA, 109
rising or have recently risen. The reason of this is, that an up-
ward bend in a stratum is resisted only by the weight of the stratum
itself, while a downward bend is resisted by the pressure on the
strata below ; so that an upward bend is more likely than a down-
ward one to become great enough to produce fracture.
3. On Some Pornts in the Groxoey of the Nurcusournoop of Maraea.
By Don M. pr Orvesa.
(Communicated by Sir. R. I. Murchison, Bart. F.R.S., F.G.8.)}
{Puarte V.]
Mvucn remains to be done in the investigation of the geological
structure of Spain. The Spanish geologists have principally de-
scribed in a general manner the mineral character of the soil
in various districts, but they have not paid sufficient attention to
the order of superposition and the character of the fossils, and
few foreign men of science have made this country the subject of
their investigations. For this reason, what we know at present
about the formations of the province of Malaga is principally
owing to the able memoir and excellent map of M. Verneuil.
However, as I believe this gentleman did not travel in the northern
part of this district, he has not given any particular description of
many geological formations which, by their order of superposition,
mineral composition, and the character of their fossils, might be of
great help in ascertaining the place in the geological scale of the
analogous strata which exist in other localities of the province,
but which do not present so many interesting data and facilities for
study. Although I am only acquainted by reference with the
opinions of this gentleman (possessing only the map he published
in conjunction with M. E. Collomb), I believe that he dwelt prin-
eipally on the Tertiary formations in this vicinity, and, above all,
on those on which the city of Malaga is built. I think that he
was the first person that ever described them, publishing also a list
of several shells, which he collected at the “ Tejares” (clay-pits in
the suburbs of this city). Professor Ansted also wrote a very valu-
able article on the Geology of Malaga, which appeared in the
‘Quarterly Journal of the Geological Society’ for 1859*. He also
paid a deserved attention to the “ Tejares” clays, which are no
doubt of the greatest interest, and described several formations in
this neighbourhood, particularly those lying on the eastern side of
the town; but I feel rather surprised to see that, while treating on
the metamorphic rocks, he does not mention the plutonic, which
are also found about here, mentioning only the serpentine of the
Sierra de Meijas, and not saying one word about the greenstone
(diorite), which is very abundant in several parts of the province,
especially in this locality, and which may have been the cause of
* Vol. xv. p. 585.
110 PROCEEDINGS OF THE GEOLOGICAL ‘SOCIETY. [Jan. 11,
the upheaval and the mammillated shape of the mountainous region
situated on the north-eastern side of this town. Neither was he
acquainted with the modern volcanic district of Riogordo; this,
however, is not suprising, as the place is out of the common track,
being situated in the centre of a mountainous region, and it has not
been brought into notice until very lately, by my friend the distin-
guished archeologist Dr. Berlanger.
But what struck me more particularly in Prof. Ansted’s memoir
was his assertion that fossils are exceedingly rare in the Secondary
limestones of the south of Andalusia, and that, although the few spe-
cimens that different geologists had been able to collect had enabled
them to agree as to the Jurassic character of the rocks, they could
not determine whether they belonged to the upper or lower division
of that period. My limited personal experience corroborated this
view; but having lately become acquainted with a Secondary for-
mation rich in fossils, and bearing a character similar in its com-
position to those which exist in several parts of the south of Spain,
I shall make its description the subject of this communication.
A couple of miles to the south of the city of Antequera, and
about thirty miles from Malaga, there exists a mountain-chain,
running from E.to W. for about thirty miles. It is very rough and
steep, and in some places attains the height of 7000 feet above
the level of the sea. Near Antequera it divides into two branches :
the one nearer to the city, in the northern direction, called Sierra
de la Chimenea, is the culminating point of the whole chain; and
the other, which is about 1000 feet lower, extends to the south-
west, sloping in that direction, while at other points it presents
nearly vertical precipices. This branch of the Sierra is popularly
called the “Torcal,’ on account of the huge blocks of stone of
which it is composed. I had long heard much about its wonderful
structure ; but, owing to its difficult access, few persons haye climbed
it, and therefore all the information I could collect was of a very
vague character. At the end of last year I determined to visit it,
accompanied by some friends.
Fancy yourself in a great city of marble, with immense squares
and numerous streets, covered with castles, arches, and pyramids,
and other buildings of the most fantastic shape and colossal
size. Such was the spectacle which developed itself before us, with-
out much strain upon the imagination. The rocks sometimes assume
the form of huge monsters; and in other places we thought they
looked human, and as if great giants were frowning upon us.
Natural bridges were seen in every direction; but what surprised us
more was the wonderful state of equilibrium in which many of the
rocks were piled together; we repeatedly saw, for example, an
enormous rock on the top of a slender pyramid, which, although
it looks likely to fall at the slightest breeze, has stood firm in this
position for successive ages. I assure you that I do not exaggerate
in the slightest degree the extraordinary magnificence of this
natural wonder. Ishould recommend all travellers who love to con-
template the beautiful and capricious forms of nature in her strangest
1871.] DE ORUEBA— GEOLOGY OF MALAGA. dat
mood to visit the Toreal, and hope that soon some abler pen may do
full justice to its merits.
As soon as our first impression had subsided, we began to.speculate
upon the causes which had made the rocks assume such a fantastic
shape. We all agreed that it must have been an effect of denuda-
tion; in what particular way, however, we could not determine,
although we were inclined to ascribe it to an ancient glacier: this
opinion appeared to acquire some support when we found, on our
descent, some rocks detached and separated a long way from the
general mass, which we considered to be erratic blocks carried
down by the action of ice. However, not being satisfied with
this conclusion, and desiring to study the phenomena of the place
with more attention, some of us returned there; and by starting
before daybreak from Antequera we were able to remain several.
hours on the Torcal, and had more time for observing the form
and composition of the rocks.
In order to convey to you the best idea that I can of these forma-
tions, I shall begin with the plain of Antequera, which, in our rapid
excursions through it, we considered to belong to the Tertiary period.
The soil of the southern part of the city consists of a dark blue
and compact limestone, in a semicrystalline state, which is over-
lapped on the northern side by a coarse and fragile rock, also
calcareous, with a certain mixture of sand, seeming to me to be
analogous to the “ Calcaire grossier” of the Paris basin. This stra-
tum dips to the south ; its thickness is rather considerable—I believe,
reaching twenty or thirty yards. It contains many fossils, prin-
cipally the casts of an Arca, which are very abundant. In the same
valley, in a place called Castillon, about three miles west of Ante-
quera, at the site of an ancient Roman town named Singilia, I have
found many fragments of a beautiful marble, entirely composed of
shells of Foraminifera—I believe, of the same kind as that which
Sir Charles Lyell describes in page 301 of the sixth edition of his
‘Elements,’ under the name of Miliolite limestone. I had no oppor-
tunity of ascertaining the position of the blocks from which these
fragments were detached; they were wrought remains of ancient
buildings ; but, considering their abundance, I came to the conclu-
sion that their quarry could not be far off. We have also in this
neighbourhood the same Miliolite limestone, in concretion with an-
other caleareous stratum, containing many Nummulites (said also to
be found near Antequera, although I have not met with them
myself) ; and it is probable that both may belong to the same period,
and that this may be either the Middle or the Lower Eocene. I see
this is also the opinion of M. de Verneuil; for in his map he classifies
the plain of Antequera as “ Tertiaire inférieure,” although he does
not seem to have found any Nummulites; for that portion of his
map does not contain the sign which indicates their presence.
Between Antequera and the Torcal there is another calcareous
formation, containing many forms of Giryphea ; it is above the blue
limestone, and of very limited extent.
The Torcal rises abruptly from the plain of Antequera, its north-
112 PROCEEDINGS OF THE GHOLOGICAL society, [Jan. 11,
ern side being very precipitous. Its formation is also calcareous.
It consists of a very compact limestone, generally of a red colour,
owing to the great proportion of peroxide of iron which it contains.
It makes a very good building-material, and has been largely employed
in the construction of Antequera. On the eastern side it reposes
in conformable stratification on a fine-grained and white oolitic
marble, which attains a considerable thickness, the extent of which I
was not able to determine with any degree of precision, although it
appeared to me that it could not be less than 1000 feet. In the
divisional line between the two formations there were many Ammo-
nites, lying in a position perfectly parallel to the plane of stratifica-
tion, andin the same place in which they were originally deposited,
without haying suffered the slightest disturbance. It is the red
marble that presents the fantastic forms alluded to before.
At the top of the ridge there are large platforms surrounded
by vertical rocks, which are scooped out horizontally in a continuous
direction, being principally grooved at their base—so much so that
in some places the top greatly projects, making the rock assume the
form of a great table, while in other places the grooving is reduced
to three or four yards above the level of the plateau, whilst the rest
of the cliff remains vertical, having the appearance of long continucus
caves. The platforms are generally perfectly plane and horizontal,
although full of crevices and faults, which are sometimes of consider-
able depth. Large angular masses of detached rocks are found in all
parts of these basins ; these, however, are more rounded; that is, their
angles are not so sharp as those of the cliffs. We received the
impression that these platforms had been the beds of ancient lakes,
the water of which had subsided at certain intervals, but not in a
gradual and uniform manner, causing certain levels to remain
longer stationary than others, the lower ones enduring the longest.
In support of this view, we found that the basins have generally
an outlet through which they have been drained, so that we could
easily trace to a considerable distance the direction of the current
as it escaped from the lake. In many of these lakes (if I may so call
them) there exist vertical caverns of great depth. The strata dip to
the south-west at a very slight angle; and the declivities of the
mountain in that direction are those which present the grandest
points of scenery. They contain an immense labyrinth of small
valleys and ravines, in the mazes of which we should have lost our-
selves had we not been accompanied by a local guide. It is in this
locality that the rocks assume their wildest and most fantastic ap-
pearance. I calculate that these windings extend for a distance of
three or four miles at the least; and the whole length of the Torcal
will be about two leagues. In its upper part, there exist veins of
laminated peroxide of iron; and on the slopes we found a great many
erystals of carbonate of lime, some of the common rhombohedral type
(calcite), while a great majority had a very fibrous structure.
This mountain-chain must have risen from the valley of Antequera;
but its upheaval must have been exceedingly gradual and gentle, as
its planes of stratification run perfectly parallel throughout, and we
Quart Journ.CGeol Soe Vol. XX\
Jesse
Milde lth M&NAanhart imp
AMMONITES FROM MALAGA.
1871.] DE ORUEBA—GEOLOGY OF MALAGA. 113
could not anywhere perceive the slightest distortion. We concurred
in opinion that it had been denuded after attaining its high level.
The mountain-chain of which the Torcal forms a part extends
in a western direction for about thirty miles. After leaving the plain
of Antequera it takes the name of “Sierra del Valle de Abdalagis,”
ending a little to the west of the place crossed by the Malaga and
Cordova Railway, named the “ Tajos del Gaitan.” In this spot the
river Guadalhorce has not only excavated a very deep and narrow
ravine, but it has actually pierced through an enormous mass of
rock at least 800 feet high, giving a further proof of the highly
disintegrable character of the rock. The scenery here is also very
wild and grand; and no traveller who passes through this defile can
be wholly free from a feeling of awe and admiration. The colour of
the compact limestone in these parts of the chain is white, having
little or no admixture of iron. However, this rock is everywhere to
be seen superposed upon the Oolite. The Jurassic strata which con-
stitute the mountainous districts to the south and west of Ronda may
belong to the same period, as well as those which exist in this
neighbourhood, about two miles west of the town, constituting
the quarries of St. Telmo, mentioned in Professor Ansted’s memoir ;
these rocks, though devoid of fossils, have a marked similarity to
those which constitute the Tajos del Gaitan. The corroboration of
these views, however, must be the result of a careful and consci-
entious study, which I have not undertaken.
Note.—This paper was accompanied by photographs of Ammonites
obtained from the compact limestone of the Sierra del Valle de Ab-
dalagis, and of one from the Sierra de la Chimenea. These Am-
monites are all of Jurassic age, and probably from the middle and
higher members of that group of rocks. Some of the specimens
represented are far too imperfect for identification; but Mr. Etheridge,
to whom they have been submitted, refers four of them to Amm.
Achilles, D’Orb. (Pl. V. fig. 1), and two others to Amm. perarmatus,
Sow., one of which closely resembles the var. catena, D’Orb. (fig. 3).
The remainder cannot safely be identified. Of the species repre-
sented in fig. 2, there are photographs of two ages.
EXPLANATION OF PLATE V.
(Figures about half the natural size.)
Fig. 1. Ammonites Achilles, D’Orb.
2. Ammonites, sp.
3. Ammonites perarmatus, Sow., var. catena, D’Orb,
Discussion.
Prof. Anstep remarked that the condition of the Torcal was similar
to that prevailing in many other limestone. districts, and was pro-
bably due to subaerial denudation.
Mr. W. W. Suyrx mentioned that he had lately had an opportunity
of examining, at Cadiz, a collection of fossils formed by Mr. Mac-
pherson in that district, which also contained specimens of Ammo-
VOL. XXVII.—PART I. I
114 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 11.
nites. It appeared that there were large tracts in which the rocks
seemed to be almost destitute of fossils, which rendered their classifica-
tion extremely difficult; and great credit was due to the author for his
exertions in a country where unfortunately so little interestis taken
in geology. He mentioned that some of these unfossiliferous rocks
had been classified as Silurian by some French geologists ; but for
this there was not the slightest evidence. It appeared far more pro-
bable that they were cf Jurassic age. Some red beds, which had
been called Triassic, were also in all probability Tertiary.
Mr. Gwry Jerrreys, who had examined several collections in Spain
and Portugal, stated that he had been much struck with the absence
of newer Tertiary fossils, the latest being of Miocene age. These
latter presented a tropical aspect, and differed from the mollusca now
inhabiting the neighbouring seas.
Mr. Brake was not satisfied with the determination of the Am-
monites, which appeared to him to be Cretaceous rather than Jurassic
forms.
Mr. Tate observed that the French geologists had determined the
existence in Spain of the whole Jurassic series, from the Middle Lias
to the Portlandian beds; and, judging from the photographs, he
should consider the Ammonites to be Middle Jurassic.
Mr. Borp Dawxins cited the remains of Rhinoceros etruscus, pro-
cured by the late Dr. Falconer at Malaga, as affording evidence of the _
presence of beds of Pliocene age in that district.
Prof. Duncan mentioned that corals of the genus Flabellum, such
as were found in the Tejares clays, had been obtained in recent deep-
sea dredgings in the Atlantic, and also occurred among specimens
brought from Japan.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
POSTPONED PAPERS.
1. On the Structure of the Crag-BEps of Surrork and Norroix,
with some OBSERVATIONS on their Orneanic Remarns. By Josepu
PxrestwicH, Esq., F.R.S., F.G.8. Part I—Tux Corattine Crae
oF SUFFOLK.
(Read March 11, 1868.)
[Plate VI.]
Previousty to 1835, although some observers, and Mr. Searles Wood
in particular, had noted the peculiarity of the fossils from the beds
now known as the “ Coralline Crag,” no stratigraphical divisions of
the Crag-beds of Norfolk, Suffolk, and Essex had been established.
In that year Mr. Charlesworth*, in a paper communicated to this
Society, showed that in Suffolk the Crag could be divided into an
Upper (the Red) and a Lower (the Coralline) Crag; and he after-
wards formed a third and higher zone of the Mammaliferous Crag of
Norfolk. With respect to the two lower divisions several cases of
direct superposition were given, which established beyond doubt
the relative position of the Red and Coralline Crags. On the other
hand, the difference between the Red and Mammaliferous Crag was
founded entirely on paleontological evidence, as no instance of
superposition was known; and although more than thirty years
have now elapsed, the question in that respect remains in the same
condition. The observations of Mr. Charlesworth were followed by
those of Sir C. Lyell} and, more lately, of Mr. Searles Wood, Jun.t,
and several other geologists; but the Red Crag has received more
attention than the Coralline Crag.
The object of this communication is to describe the physical
structure of the several Crags, and to determine, if possible, the exact
relation the Suffolk Crags bear to the Crag of Norfolk. With this
object in view, I have examined on several occasions the coast-
section from Aldborough to Weybourne, and the various inland
pit- and railway-cuttings, of all of which latter I took notes during
the construction of the Great Eastern Railway. The greater part
of my observations date, in fact, so far back as from 1845 to 1855,
which will explain the variation in some of the coast sections, and
account for the disappearance of some inland sections. The difficulty
of obtaining direct evidence showing the relation of the Mammali-
ferous Crag of Norfolk to the Red Crag of Suffolk, and of correlating
the beds beneath the Boulder-clay with the other beds of the same
age through the south of England, led me to delay bringing this
* Proc. Geol, Soc. vol. ii. p. 195.
t Proc. Geol. Soe. vol. iii. pp. 126 & 437, and Mag. Nat. Hist. 1839, p. 313.
¢ Ann. & Mag. Nat. Hist. for March 1864.
i)
116 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
paper forward until I was in possession of facts which might afford
sufficient grounds for the conclusions I now venture to submit to the
Society. The whole question is intimately connected; yet, as the
geological series is divisible into distinct stages, I will take each of
these separately, commencing with the lowest.
Coralline Crag.—The area of the Coralline Crag has not been
extended since Mr. Charlesworth first drew attention to it, giving
the neighbourhood of Orford as its centre, with outliers at Aldbo-
rough, Sutton, Ramsholt, and Tattingstone. The boundaries only are
better known. The extent of superficial area exposed is about eight
square miles. Originally the Coralline Crag may have extended
uninterruptedly from Aldborough to Tattingstone; but, with the
exception of the low range of hills extending from Gedgrave north-
ward to Orford, Sudbourne, and Iken, and the small outlying masses
of Aldborough, Sutton, and Tattingstone, it has everywhere been
removed by denudation. Not only did this denudation remove the
Coralline Crag, but it has also removed a portion of the underlying
London Clay; so that the base of the Red Crag is in places lower
than that of the older Coralline Crag, round and over which it
wraps and passes transgressively.
The surface of the London Clay under the Coralline Crag is also
uneven. In the Bullock-yard pit, on Mr. Colchester’s farm at Sut-
ton, it is found under 4 feet of Red and 2 of Coralline Crag, and
20 feet above high tide of the river Deben; but an eighth of a
mile to the west the London Clay is 12 feet lower, and a lower
zone of the Coralline Crag comesin. This and other circumstances
lead me to believe that at the noted old pit at Ramsholt the Coral-
line Crag, which there lies on the London Clay, does not belong to
the lowest zone, but to one some 10 to 15 feet higher.
The well-known outlier of Sutton supplies us with a typical
exhibition of the Coralline Crag, the several pits which have from
time to time been opened there giving us the best clue to its structure
and dimensions, whilst at the same time the extent of denudation by
the Red Crag, and the varying levels of the sea during the deposition
of these latter beds, are well shown (see Plan and Sections, Pl. VI.).
It is generally known that the Coralline Crag consists of two
divisions—an upper one, formed chiefly of the remains of Bryozoa,
and a lower one of light-coloured sands, with a profusion of shells.
The more exact dimensions and subdivisions of these beds at Sutton,
Orford, Sudbourne, and Gedgrave I now purpose to give.
The discovery of the so-called Coprolites in the Red Crag by the
late Professor Henslow, in 1848, led to a great extension of crag-
pits. With one exception they were all in the Red Crag. The only
one in the Coralline Crag was opened by Mr. Colchester, on the
south side of Sutton-farm Hill (a, Pl. VI.).. Unfortunately the pit did
not prove remunerative, and a year or two later it was filled up, and
the ground levelled ; so that it was only.seen by myself and Mr. Ray
Lankester, as mentioned by him in a paper read before this Society.
The section was of much interest, as it exposed beds which belong,
I believe, to the lowest zone of the Coralline Crag, and showed
°
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 7
a basement bed with fossils and boulders of an unexpected and
remarkable character (fig. 1).
Fig. 1.—Section of old pit on Mr. Colchester’s farm, Sutton.
Feet.
Surface soil.
1
Ne White marly sands with seams of Cyprina.
17
c. Ditto with Mya and Bryozoa in lower part,
and Curdita, Astarte, Anomia, and Venus
common in upper part.
of Cyprina, Pecten, Cellepora cespitosa, &e.
\
|
|
|
{
|
|
}
te Bed of comminuted shells, with single valves
a.
Bed of phosphatie nodules, with mammalian
and cetacean remains, and foreign boulders.
London Clay.
(Unless mentioned to the contrary, all the pit-sections in this paper are on
the same scale, viz. 12 feet to the inch vertical.)
The surface of the London Clay is here 8 feet above high-water
level of the adjacent river Deben. Immediately on the London Clay
we find a bed, from 1 to 14 foot thick, of phosphatic nodules, not to
be distinguished in general appearance from those of the Red Crag.
Among them I found, as in the Red Crag, a great many fossil
Crustacea, much worn, derived from the London Clay, and consisting
of the following species :—
Archzocarabus Bowerbankii. Scyllaridia Keenigi.
Dromolites Bucklandii. Thenops scyllariformis.
Hoploparia Bellii. Xanthopsis Leachii.
—— gammaroides. Xantholithes Bowerbankii.
With these I found one fragment of the horn of a Deer much mine-
ralized, a small Cetacean vertebra retaining the ordinary bone-
structure, together with numerous teeth of sharks. In the same bed
were worn blocks of Septaria from the London Clay, drilled by boring
mollusca, and flat, worn, highly mineralized Cetacean bones, super-
ficially punctured, as those in the Red Crag, together with fragments
of Bryozoa, Terebratula grandis, and Cyprina, much worn, and the
latter full of the cavities made by minute boring sponges. With these
organic remains there were a small number of the nodules or balls
of coarse dark-brown sandstone, often containing the cast of a shell,
so common in places in the Red Crag; there were also small pebbles
of quartz and of flints, and some large pebbles of light-coloured,
hard, siliceous sandstone: but the most remarkable specimen I there
found was a rounded boulder of dark-red porphyry of considerable
size, and weighing about a quarter of a ton. None of the specimens
were angular or striated.
On mentioning these circumstances to Mr. Colchester, I found
118 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
that he and his son had made a valuable collection from this pit,
which he at once kindly placed in my hands.
; The following is a list of the principal and more important spe-
cimens thus obtained.
One tooth of Mastodon (M. arvernensis)*.
Two teeth of Rhinoceros (2. Schlecermacheri?) ; both milk-teeth.
Two teeth of Deer (Cervus dicranoceros).
Four teeth of Cetaceans.
One vertebra of Whale, large.
Two ear-bones of Whale; one mineralized, the other not.
Four skulls of Belemnoziphius.
Many teeth of Carcharodon and Lamna.
One vertebra of a Saurian (an extraneous fossil of Jurassic age).
These are fossils identical with the species from the Red Crag ; and,
like them, they present a highly mineralized condition, and are,
with the exception of some of the Cetacean and a few of the other
Mammalian remains, all more or less rolled, worn, and polished.
Over this nodule-bed are about + feet of finely comminuted shells,
with a few single valves of Pecten, Cyprina, Mactra, together with
Turritella and Terebra, and then 17 feet of light-coloured marly
Crag, abounding in large shells and with few Bryozoa. In the
lower part of this bed were some specimens of the Mya truncata,
in the position in which they lived; the Cyprina islandica, var.,
sometimes double, was common in certain layers; and in the upper
part of the bed Anomia, Astarte, Diplodonta, and Venus abounded,
together with a variety of Foraminifera, whilst univalves were com-
paratively scarce. They had ceased working this pit when I visited
it in 1861 and 1862 ; and on my returning at a later period, hoping to
make a more complete collection of the shells, I found it levelled down.
It is probable that part of bed ¢ of this section is synchronous
with the crag of the small Ramsholt pit, which yielded so large a
number of rare and beautiful fossils to the researches of Mr. Charles-
worth, Sir Charles Lyell, and Mr. Colchester. Many species were
more abundant at Ramsholt than in any other locality, and were
generally in a very fine state of preservation—the bivalves often
with both valves. Among the commoner species were Cardita
senilis, Cyprina islandica, Pecten maximus, P. opercularis, Panopea
Fawjasii, Astarte Burtini, A. gracilis, Trochus zizyphinus, T’. conulus,
and the large Balanus concavus. The latter occurred in hundreds.
This bed is also characterized by Cytherea chione, Hinnites Cortesyr,
Lima hians, Tapes perovalis, Natica proxima, N. varians, N. cir-
riformis, Pyrula reticulata, Balanus bisulcatus, Pyrgoma anglica,
Spatangus purpureus, Brissus scille, Flabellum Woodii, and several
species of Echinus and Temnechinus.
The upper part of the section at this pit (fig. 1) seems to be on the
level of that part of the Coralline Crag which is under the Red Crag
in the Bullock-yard (p, Pl. VI.). It may be seen by digging through
the 2 to 4 feet of Red Crag forming the floor of the pit. It was full
of Cardita, Pecten, Astarte, and various characteristic shells of the
* Mr. Lankester says, however, ‘‘a Mastodon.tooth which I have seen from
that situation is not M. arvernensis, but belongs to the Trilophodont species.” —
Quart, Journ. Geol. Soe. vol. xxvi. p. 497.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 119
Coralline Crag. It is on the side of this old yard, and therefore im-
mediately above the bed with Cardita &c., that the Coralline Crag rises
in an old cliff well described by Sir Charles Lyell *, and to which I
shall have occasion to refer again. The lower part of this cliff con-
sists of light-coloured sands (¢), with a few Bryozoa and a good many
small shells ; while the upper part (part of f) is composed in great part
of comminuted shells. No higher bed is seen here; but on the other
side of the hill, and at a distance of 400 feet west of this pit, is an old
quarry, which, when I first visited it in 1836, had recently been ex-
tensively worked for rubble to form the river-wall. In the lower part
of this pit (fig. 2) the bed of sand e¢, just referred to in the Bullock-
Fig. 2.—Section in old Quarry, Sutton. Top of hill overlooking the
Deben. (See Fr, Map and Sections, Pl. VI.)
Surface soil.
=. /Y Dark ferruginous beds of Bryozoa, mostly
in fragments, some entire, with a few
shells in the same state. White soft
calcareous veins descend through these
beds from the top. 11 feet.
f Fine sand and grit, comminuted shells,
numerous small perfect shells, and
some Bryozoa. 6 feet.
Uniform fine compact sand, with small
shells and Bryozoa in the position of
growth. 4 feet.
yard pit, is well exposed. It is 12 feet thick, and consists of a light
yellow sand, with a few shells, mostly small or young individuals, with
a number of Bryozoa in a fine state of preservation and mostly in the
position in which they lived. In some places these Bryozoa are very
numerous, and arranged in regular but not continuous bands, like
flints in the Chalk. The prevailing species are Cellepora coronoporus,
Eschara porosa, and other species of Cellepora and Eschara,a species of
Certopora, and another large branching species. Many of these are 1n
the most beautiful state of preservation and perfectly uninjured. They
are now, however, best seen in a small section between the large pit
or quarry and the cottages at the entrance to the Bullock-yard.
Overlying these sands with undisturbed Bryozoa is a bed, f, from
5 to 8 feet thick, consisting of comminuted shells with seams of
oblique lamination, containing a few Bryozoa, and with a consider-
able number of shells, also mostly small or young individuals, in a
good state of preservation. Intercalated in this bed are several
finely laminated indurated irregular seams of yellow marl or lime-
stone, containing small shells, Foraminifera, and some rare species
Op. cit.
120 PROCKEDINGS OF THE GEOLOGICAL SOCIETY.
of Bryozoa, including the Salicornaria sinuosa, which I found here
in greater abundance and more perfect preservation than at any
other spot. It also contains dark green grains of silicate of iron,
dispersed andin seams. The globose Fascicularia and Alveolaria are
common in both e and f.
In strong contrast with this lower bed is the overlying ferruginous
soft rock, which forms the upper part of this quarry. It consists
essentially of comminuted shells and of fragments of Bryozoa, and
often shows oblique lamination. This mass, which here is about
11 feet thick, is cemented together, partly by carbonate of lime, and at
this spot partly by the oxide of iron, and forms a soft and very porous
dark brown rock. Detached valves of Pectens and other shells, and a
considerable number of Fascicularie and Alveolarie are found entire,
together with remains of Crustacea and Echinodermata. This bed at
Sutton is but 11 feet thick, forming only the lower part of the
upper division of the Coralline Crag. It is more largely developed
in the neighbourhood of Sudbourne, where it attains a thickness of
20 feet. At Low Gedgrave there is a pit where it is nearly 30 feet
thick. This division of the Crag often presents numerous curious
instances of oblique lamination, and exhibits, in fact, a very in-
structive illustration of the frequent reconstruction of old shell-
banks. Altogether the series of beds at and around Sutton and
Sudbourne, especially some in the near vicinity of Sudbourne church
(as in fig. 3), are of the greatest interest.
Fig. 3.—Pit 5 furlongs E.N.E. from Sudbourne Church.
Ww. eee
Beds of comminuted shells and of Bryozoa forming a soft building-stone.
This division is generally very uniform in its composition. There
is a pit, however, at the corner of the two cross-roads, 6 furlongs
N.N.E. from Sudbourne Church, where the upper 6 feet consists of
finely comminuted shells, with a few Bryozoa.
This completes the series of beds forming the two divisions of the
Coralline Crag. I have denoted them by letters, for the convenience
of correlation with the same beds in other parts of the district.
The thickness of the lower division of the Coralline Crag, as proved
at Sutton, is about 47 feet, and that of the upper division, as it
exists in the neighbourhood of Sudbourne and Gedgrave, about 36,
making a total of 83 feet.
Taking the whole together, the general section of the Coralline
Crag is as follows (fig. 4) :—
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 121
h. Sand and comminuted Sudbourne.
shells.
Gedgrave.
sisting almost entirely é
of comminuted shells Sudan he.
andremainsof Bryo- Gedgrave.
\% A series of beds con- Sutton.
|
: zoa, forming a_ soft
= building-stone. False TES
: stratification and ob- Aldbro’.
lique bedding are its
constant characters.
Upper Division, 36 feet.
SE )
entiresmall shellsand Iken.
seams of comminuted Sudbourne.
shells. Gomer.
= Sand with numerous Sutton.
Bryozoa, often in the a
original position of Broom Hill.
growth, and some
small shells and
Echini.
Sands with numerous Sutton.
Fig. 4.—General Section of the Coralline Crag.
upper part. Thon
of limestone in the Sudbourne.
Tattingstone.
Lower Division, 47 feet.
c. Marly beds hie nu- Sutton.
merous well-preser-
ved and double shells, Ramsholt.
often in the position
in which they lived.
|
|
= be Comminuted bells, Sutton.
large entire or dou- a
= Bie shells and bands Broom Hill.
6. Comminuted shells, Sutton.
Cetacean remains,
Bryozoa.
a. Phosphaticnodulesand Sutton.
mammalian remains.
122 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Near Aldborough the upper division of the Coralline Crag, but
with more shells than at Sutton, is alone exposed. It contains casts
of Voluta Lamberti, of Cyprina islandica, with specimens of Kchini
and Crustacea. Of the latter, a beautiful specimen referable, ac-
cording to Mr. H. Woodward, to the genus G'onoplaw, and probably
to G. angulata, Leach, was found by my young friend Mr. Norman
Evans.
At Iken brick-yard and some adjoining pits the same upper divi-
sion with Bryozoan remains is found; while in the lower ground,
between the brick-pit and the church, and again between the
Brick-pit and Webber’s-Whin Farm, the upper bed f of the lower
division (which is here more developed than at Sutton, and con-
tains some thin seams of hard shelly indurated limestone) crops
out. In the numerous pits in the neighbourhood of Sudbourne
Church the upper division g is alone exposed ; but it is now rarely
quarried.
In Sudbourne Park there is a pit on the higher ground which shows
a good section of the Bryozoa-beds of the upper division ; while a small
shallow pit in the low ground close by the Hall has been long noted for
the beauty and variety of its fossil shells. Cyprina, Astarte, Cardita,
and Terebratula, &c. abound in this pit, which belongs, I think, to
part of bed d (see general section, fig. 4).
Fig. 5.—Pit on Broom Hill, near Keeper's Lodge, 1 mile W. from
Orford Church.
ects Surface and Drift Soil.
=== ¢. Yellow Sand full of Fascicularia,
Alveolaria and Cellepora; few shells.
d. Sandy beds with comminuted shells,
thin bands of tabular limestone,
layers of large and entire shells and
a few Bryozoa. The lower bed is
full of fine entire Cyprine, Thracie,
Panopee, Diplodonte, Terebratule,
and Cardite, often double.
15
The well-known pit by the keeper’s lodge at Broom Hill, Ged-
grave (fig. 5), shows 7 or 8 feet of yellow sands, full of detached
Bryozoa, chiefly Fascicularia and Alveolaria, belonging to the
zone ¢; beneath this are 15 feet of comminuted shells, interca-
lated in which are seams of large shells in a fine state of preserva-
tion. In the lower part of this pit, some of the semiindurated
seams, when broken open in the plane of bedding, are found studded
PRESTWICH——CRAG=BEDS OF SUFFOLK AND NORFOLK. 123
with magnificent specimens of Cyprina islandica, Mya truncata,
Panopea Fawasii, various species of Astarte, Cardita, Venus, and
other shells. These beds belong to the zone d *.
At Low Gedgrave, there is a shallow pit near the farm-buildings,
showing a section composed of layers of comminuted shells with
irregular seams of shelly limestone and sand, in which a number of
* As showing the importance of keeping each stratum separate, I give two
special lists of specimens collected by my friend the late Dr. Woodward during
a residence of some weeks in the district. In the one case (Broom Hill) the
fossils of zone d (including parts of e), and in the other (Gomer) those of zone f,
thus appear as distinct groups.
CorRAuLine Craa.
Keeper’s-Lodge pit, Broom Hill (near Orford).
(Bivalves abundant ; univalves comparatively scarce. Authority, S. P. Wood-
ward, from specimens collected in 1863.)
Cypreea europa.
Buccinum undatum.
Turritella incrassata.
Sealaria subulata.
clathratula.
Rissoa crassistriata.
Czcum mamillatum.
Trochus zizyphinus.
formosus.
Margarita trochoidea.
Adeorbis striata.
Natica proxima.
Calyptrea chinensis.
Emarginula fissura.
Fissurella greeca.
Anomia ephippium.
striata.
Ostrea edulis.
Pecten maximus.
= Gerardil.
tigrinus.
pusio.
opercularis (very abundant).
Lima Loscombii.
Pinna pectinata.
Mytilus hesperianus.
Crenella sericea.
Pectunculus glycimeris (abundant).
Limopsis aurita.
Nucula nucleus.
Leda semistriata.
Lucina crenulata.
borealis (abundant).
Diplodonta rotundata.
Lucinopsis Lajonkairi.
Verticordia cardiiformis.
Cardium strigilliferum.
decorticatum.
Cardita senilis (abundant).
scalaris (abundant).
Cardita orbicularis.
corbis.
, var.
Astarte Basterotii.
mutabilis.
—— Omalii (very abundant).
—— gracilis.
Burtinii.
Cyprina islandica (very abundant).
rustica.
Cytherea chione.
rudis.
Venus imbricata.
casina (abundant).
ovata.
Psammobia ferroénsis.
Tellina obliqua.
donacina.
Mactra arcuata.
Solen ensis.
Thracia inflata.
ventricosa.
Corbula nucleus.
Mya truncata.
Panopza Faujasii (abundant).
Glycimeris angusta.
Lingula Dumortieri.
Terebratula grandis (abundant).
Spirorbis.
Balanus crenatus.
Blumenbachium globosum.
Fascicularia, sp.
tubipora.
Cladocora cariosa.
Turbinolia Milletiana.
Echinus Woodwardi.
Spatangus.
Discoporella.
Heteropora pustulosa.
124 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
rare small fossils have been found: this bed either belongs to part
of zone d, or may possibly be an expansion of zone f. The same
Lunulites conica.
Hornera reteporacea (infundibulata).
striata.
Eschara monilifera.
Cupularia canariensis.
Gomer (a small temporary pit in a field between Low Gedgrave and Broom Hill,
but on slightly higher ground than the latter).
(Very rich in species, univalves and bivalves. Authority, S. P. Woodward,
from specimens collected in 1863.)
Ovulum (Leathesii) spelta ?
Cyprea retusa.
europea.
Hrato leevis.
Maugeriz.
Voluta Lamberti.
Mitra ebenus (Mr. Evans ?).
Aporrhais pes-pelicani.
Terebra inversa.
canalis.
Cassidaria bicatenata.
Nassa labiosa.
granulata.
—— consociata.
prismatica.
Buccinum Dalei.
undatum, var.
Murex corallinus.
Triton heptagonum.
Fusus gracilis, var. propinquus.
alveolatus.
consocialis.
Trophon muricatus.
Pleurotoma porrecta.
semicolon ?
, var.
Mangelia castanea.
—— perpulchra.
costata.
mitrula.
eancellata.
Bela concinnata.
Cancellaria mitrzeformis.
scalarioides.
Cerithium trilineatum.
tuberculare, var.
adversum.
granosum.
Turritella merassata.
Pyramidella lzviuscula.
Chemuitzia, n. sp.
elegantissima.
Odostomia plicata.
truncatula ?
Scalaria varicosa.
frondicula.
— foliacea.
subulata.
clathratula.
Scalaria? cancellata.
Kulima subulata.
Rissoa confinis.
obsoleta.
Czcum mamillatum.
glabrum.
Lacuna reticulata.
Trochus zizyphinus.
, var. monstrosus.
granulatus (papillosus).
millegranus.
— villicus ?
—— Adansoni.
—— Kicksii.
- tricariniferus.
obconicus.
Margarita ? maculata.
trochoidea.
Adeorbis striatus.
supra-nitidus.
pulchralis.
Natica proxima.
varians.
cirriformis.
multipunctata.
Pileopsis ungaricus.
Calyptrza chinensis.
Emarginula fissura.
crassa.
Bulla lignaria.
conuloidea.
Cylichna cylindracea.
Dentalium costatum.
bifissum.
Anomia ephippium.
striata.
Ostrea edulis.
Pecten maximus.
—— Gerardii.
similis.
tigrinus.
—— pusio, var. striata.
—— opercularis.
, var.
Lima exilis.
subauriculata.
Pinna pectinata.
Modiola phaseolina.
marmorata.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 125
sand and flaggy limestone is worked ina pit a few yards to the south-
east of the barm at the extreme south-west point of Gedgrave Hill.
The shelly beds, with flags of shelly limestone at Tattingstone (see
section in Part II.), may possibly be referred also to zone d.
With regard to the bed of phosphatic nodules, it is no longer
exposed at Sutton, and it has not been reached in any of the pits in
the neighbourhood of Orford; but there is a shallow pit now worked
between Butley Abbey and Butley River, which may probably be-
long to the base of the Coralline Crag; the crag-beds themselves
have been removed, with the exception of a foot or two, which is so
disturbed as to render its identification doubtful. Still, from the
abundance of Cardita senilis, Astarte Omalii, and Cyprina islandica,
the occurrence, although rare, of Mytilus hesperianus, Pecten maat-
mus, and Isocardia cor, and the absence of the ordinary shells of
the Red Crag, with the exception of a few specimens of Trophon
antiquus, near the surface, I should feel disposed to consider this
a disturbed portion of the Coralline Crag, and to refer the 2-foot
coprolite-bed below it to this formation.
Orgame Remains.
The Mollusca of the Coralline Crag have been worked out by Mr.
Searles Wood with so much skill and perseverance that there is little
Pectunculus glycymeris. Astarte Burtinii.
Limopsis aurita (rare). ? digitaria.
pygmea. parva.
Nucinella miliaris. Cyprina islandica.
Arca pectunculoides. rustica.
Nucula levigata, var. Circe minima.
tenuis ? Cytherea rudis.
nucleus. Venus imbricata.
Leda pygmza. casina.
Kellia ambigua. ovata.
: —, large var.
Montacuta bidentata.
truncata.
—— substriata.
ferruginosa.
Cryptodon sinuosun.
Lueina borealis.
Diplodonta rotundata.
dilatata.
Cardium nodosum.
—— strigilliferum.
—— decorticatum.
Cardita senilis.
scalaris.
—— orbicularis.
corbis.
==, he
Erycinella ovalis.
Astarte triangularis.
parvula.
Basterotii.
—— mutabilis.
—— Onmallii.
—— gracilis.
Gastrana laminosa.
Donax politus.
Tellina obliqua.
donacina.
Syndosmya prismatica.
Mactra obtruncata.
triangulata.
Lutraria elliptica.
Solen ensis.
Thracia phaseolina.
inflata.
Pholadomya hesterna (?).
Corbula nucleus.
Saxicava ? carinata.
Glycimeris angusta.
Terebratula grandis.
Ditrupa subulata.
Balanus concavus (retaining colour).
bisulcatus (common on Lucina
and Pecten Gerardi1).
Cellepora edax.
Hornera infundibulata.
Cupularia porosa.
126 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
chance of any observer adding to his list without being able to devote
very much more time to the subject than I have had at my disposal.
There is certainly no formation in England, and probably none
abroad, the fossils of which have been the object of researches more
assiduous and more conscientiously made than those of Mr. Searles
Wood. Not only has Mr. Wood formed collections rarely equalled
in their completeness and extent, but he has also ably described and
illustrated them in the early volumes of the Paleontographical
Society*. The other organic remains of the Crag have also been
described in the same work by most competent authorities in the
different natural-history sections in the following order :—
Mollusca, by Mr. Searles Wood (Palxontogra-
phical Society's Monographs‘)............-..-+- 1848, 1850, 1856
Corals, by MM. Milne-Edwards and J. Haime.. 1850
Girripedia iby Mir) Darwin) sa.-neee ene eee 1851, 1854
Brachiopoda, by Mr. Davidson..................... 1852
Kehinodermata, by Mr. Edward Forbes ......... 1852
Entomostraca, by Mr. Rupert Jones............... 1856
Polyzoa (Bryozoa), by Mr. Busk .................. 1859
Foraminifera, by Messrs. Jones and Parker...... 1866
We are thus, with the exception of the Mammatia, which are
only of recent discovery in the Coralline Crag, furnished with a very
complete exposition of the fauna of this formation ; but there is still
work to be done in defining more exactly, by careful collections on
the spot, the fossils of each particular zone. In zones d and f this
has been partly done. Zone c is typified at Ramsholt, and may be
characterized by its Echinoderms and various large Testacea (see
list), as zone é is by its profusion of Bryozoa.
Mollusca.—So large a proportion of the shells of the Crag are
of recent species that we are furnished with unusually good data
for investigating the conditions under which this deposit was
formed, by the study of the geographical range and distribution
of those living species, and of the zones and depths through which
they range. The tendency of natural history at present is rather
to extend and remove the barriers of special zoological provinces.
Mr. Gwyn Jeffreys remarks + :—“ It seems to me, after a long
and careful study of the question, that no more than two groups
(which are apparently distinct from each other) can be recog-
nized in a geographical point of view; and for these I would sug-
gest the general but not inappropriate names of ‘ Northern’ or
‘ North-European,’ and ‘ Southern’ or ‘ South-European.’” And he
adds that “it is extremely difficult to fix the limits of even those
comparative areas of distribution; but the ‘facies’ of each group is
manifest to some extent in the littoral or shallow-water species.”
To these groups, or divisions, Mr. Jeffreys adds a third, viz.
* I am happy to hear from Mr. Wood that he is engaged upon a supplement
to his original work.
+ Last year (1870) the first part of Prof. Owen’s ‘ Fossil Cetacea of the Red
Crag’ was added to this series.
{ British Conchology, i. introd. p. lxxxvi.
PRESTWICH——CRAG-BEDS OP SUFFOLK AND NORFOLK. 127
“Oceanic, or occasional visitants.” ‘‘ The first of these divisions
corresponds with the ‘ Arctic’ and ‘ Boreal’ types of Forbes and
Hanley ; and the second to their ‘ Atlantic’ and ‘ Lusitanian’ types.
Their ‘South-British,’ ‘European,’ ‘Celtic,’ and ‘British’ types
indicate mixed or neutral ground, and partake both of northern and
southern characters.” The high authority of Mr. Gwyn Jeffreys
would induce me to adopt this broad division; but for geological
purposes, such as tracing the old land-margins, the old sea-areas,
and other questions connected with the physical geography of former
periods, I think it desirable to look at the subject more in relation
to existing continents and sea-margins. I have therefore retained
the term “ Arctic” for the species living on the Spitzbergen or
Greenland coasts, ‘‘ Scandinavian ” for the species frequenting the
coasts of Norway, Sweden, and Denmark, “ British’’ for those of the
seas immediately surrounding Great Britain, ‘““ West European” for
the species frequenting the coast of Europe from France to the Straits
of Gibraltar. Although Mr. Jeffreys has shown that the Mediter-
ranean moliuscan fauna cannot be considered distinct from that
of the East Atlantic, I have retained the Mediterranean area as
a separate province, in consequence, not so much of its exist-
ing fauna, as of the relation of that fauna with the fauna of the
later or recent Tertiaries of Italy, France, and England—a relation
of the most marked character. For the species which have a more
southern range and are found on the shores of Madeira, the Canary
Isles, and the Azores I use the term “ Mid-Atlantic.” To this an-
other region is now added, embracing the great depths of the
Atlantic generally—depths from 1200 to 15,000 feet.
Mr. Searles Wood described 322 species of Coralline-Crag Mol-
lusea, which, with the 5 species of Brachiopoda described by Mr.
Davidson, gives a total of 327 species. The late Dr. Woodward,
basing his calculations on these lists, was of opinion that the
number of extinct species was 159, and of recent species 168, which
gave a percentage of 51 of recent species. Of the latter he con-
sidered that 139 were still to be found in British seas, whilst
27 were now confined to southern and 2 to northern seas *.
The great extension of the field of research by means of deep-
sea dredging, however, has brought to light facts which render a
review of the relation of the fossils of the Crag to living species desi-
rable. Several species which were then supposed to be extinct have
since been found living; and other links have been found which
tend to show that some of the species supposed to be distinct may
be considered merely varieties of others; and I am glad to have
* Sir Charles Lyell’s ‘ Antiquity of Man,’ 1863, p. 209. In his ‘ Student's
Elements of Geology,’ p. 178, just published (1871), Sir Charles Lyell has re-
vised these lists as under :-—
Percentage
Total Not known of shells
number. as living. not known
Tesh tally elspa oon dsnanansac’ UG vee ances 47 as living.
Univalves ............... Ite Se eeeeere 60 } 315.
Brachiopods ............ Dye srabaa se 3
128 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
the opportunity of recording the opinion of another distinguished
naturalist, Mr. Gwyn Jeffreys, who has made European conchology
his especial study, and has particularly worked out the deep-sea fauna
with a view to a comparison with fossil species upon this question.
We have visited the Crag district together ; and he has examined all
the more important Crag collections, while with the same object in
view he has also extended his researches to the Pliocene collections
of the Continent. ‘The special results of his elaborate inquiry will
be found in the tabular list, pp. 137-146. The list of Coralline-
Crag Mollusca so revised gives a total of 316 species, of which Mr.
Jeffreys considers 264 to be living and 52 extinct, thus giving a per-
centage of 84 recent, and apparently only of 16 extinct species *.
Of these 265 living species of Mollusca, Mr. Jeffreys has deter-
mined 185 to be still living in the British seas, and 80 to be species
living now only in extra-British seas. Of the latter, 14 species live
in northern seas only, 65 in southern only, and 1 lives in both nor-
thern and southern seas. Dividing the living species into zoological
provinces, I find their distribution is as under :—
Bivalves. Univalves. Total. Peculiar. —
Av etl chiwss. acd cossectne see 1S oer are Wipe secete Of. suas
Scandinavian ............... 1B Aesop (ai Danae diy eevee 0
British) see cee see HOU 2a 28: 84 0... WS Jasna 2
West Huropean............ JOM ec. Seis UG ce eee 1
Mediterranean ........ ..- NOS Peeeeeee Oi oxeotiee OO mene 17
Mid-Atlantic ............... A0f ose. HAO) Wey oeee QO ade 4
Deep Atlantic............... Be sacs 5 > onoade 92) orc)
, Special localities—North America, 2; Africa, 4; West Indies, 2; Gulf of
Mexico, 1; Japan, 3.
Of the 5 species of Brachiopods in the Coralline Crag, 1 only is
extinct. Two are British species with an extensive range. Mr.
Gwyn Jeffreys has dredged the Argiope cistellula in from 20 to 80
fathoms water; and the Terebratulina caput-serpentis ranges from
the shore to 632 fathoms. The Discina atlantica has been dredged
in the deep Atlantic (7560-13,500 feet). The Lingula Dumortiert
has been dredged in the seas of Japan. As a rule, Brachiopoda may
be considered to indicate deep water.
Bryozoa.—According to Mr. Busk, there are not less than 95 species
of Bryozoa found in the Coralline Crag ; 30 of these species are now
living, and 65 are extinct. Of the former, 26 still inhabit the British
seas ; and of the other four, 3 are found on the west coast of Africa
and at Madeira, and 1 is probably living in the Australian seas. Of the
26 British species, 9 have a southern range, some as far as Patagonia
and the Falkland Islands. There is one remarkable exception to
this southern character ; the Retcpora Beaniana has been found on
the coast of Norway by Mr. M‘Andrew, and in the Arctic sea by Sir
Edward Belcher. Mr. Busk considers it to be a wholly northern
* Whether or not the greater number of shells will prove to be living, re-
mains for future research; but certainly the conclusions of Mr. Jeffreys are in
harmony with the inquiries of Sir Charles Lyell, which have shown a smaller
percentage of extinct species in the Coralline Crag of late than formerly.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 129
species*. Alcide D’Orbigny + states that he has dredged Bryozoa at
a depth of 160 metres off Cape Horn, and he considered the sea-bed
there to be formed of dead and living Bryozoa. In many places the
banks of Newfoundland are, in his opinion, covered entirely with
similar débris, Celleporat being especially abundant. The conditions
most essential to the growth of Bryozoa, according to the same
experienced observer, are :—first, considerable depth of water;
secondly, clear and limpid water ; thirdly, water constantly agitated
by waves and deep currents. 13 out of the 26 British species found
in the Coralline Crag belong to the genus Lepralia. According to
Dr. Johnston§, the greater number of these species are found in
deep water; and Mr. Busk mentions that the Lepraha ciliata has
been dredged at 45, the L. Peachii at from 110 to 147, the L. hya-
lina at from 4 to 40, and the Z. Maluszi at 48 fathoms.
Amongst other common genera of the Crag are Jdmonea and
Retepora, which may be considered essentially characteristic of
rather deep seas. The Hschare, again, live in deep water and among
strong currents. One extinct species of this genus, the #. monili-
fera, is the abundant and characteristic species of the Coralline
Crag. Another common species is the Biflustra delicatula, now to
be found only in the seas of Australia and Manilla. The curious
globose genera Alveolaria and Fascicularia are extinct, and peculiar
* Mr. Busk, however, has recently informed me that, from an examination
of the Bryozoa collected in the Mediterranean in the late voyage of the ‘ Porcu-
pine,’ he believes that &. Beaniana occurs in that sea. He has also furnished
me with the following lists of Crag species now living in the Mediterranean
and Adriatic, or fossil in the Italian Pliocene beds :—
Crag species living in the Crag species occurring in the
Mediterranean. Italian Pliocene.
Salicornaria sinuosa. Lepralia ansata.
Lepralia annulata. » Bowerbankiana.
» ansata. » Brongniartii.
» Brongniartii. » ciliata.
» Ciliata. » innominata.
» Innominata. » Malusii.
» Malusii. » mamillata.
» Morrisiana ? » Morrisiana ?
» Pallasiana. » Pallasiana.
», unicornis. » unicornis (tetragona, Heuss).
» violacea. », violacea.
Retepora cellulosa. Retepora cellulosa.
Cupularia canariensis. Cupularia canariensis.
Patinella patina. Membranipora andegavensis.
i ocean.
Lacroixii.
”
Biflustra delicatula.
Cellepora coronopus.
bs ramulosa.
» Scruposa.
» tubigera.
+ Annales des Sciences Naturelles, 1851, p. 295.
¢ The curious Cellepora edaxis often found covering, as a mantle, several spe-
cies of univalve shells.
§ History of British Zoophytes. London, 1847.
VOL. XXVIL.—PART I. K
130 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
to the Coralline Crag. Of the species and genera of Bryozoa inha-
biting shallow water, there is a marked absence.
The Bryozoa make their appearance in the lowest bed of the
Coralline Crag. I found species of Cellepora and HEschara amongst
phosphatic nodules at the base of this deposit. At Ramsholt the
Cupularia denticulata, C. canariensis, and other species were met
with. In ascending order they become gradually more numerous,
and in zone “¢” they attain a large development and, further,
occur in the position and place of growth. ‘The species seem some-
what gregarious. At Sutton we find chiefly species of Cellepora and
Eschara in this bed, whilst at Broom Hill little else is found but the
various species of Fuscicularia and Alveolaria and some Cellepora.
In the highest bed, “ f,” of this division, where extremely fine sedi-
mentary seams are intercalated with a mass of comminuted shells,
the delicate Salicornaria sinuosa seems to have flourished.
The upper division of the Coralline Crag, as is well known, is
composed to a great extent of fragments of Bryozoa and com-
minuted shells, with a certain number of entire Alveolarie and Fas-
cicularie and shells. As the structure of these beds shows them to
have been subjected to the action of shifting currents and frequent
reconstruction, it is probable that these banks of Bryozoan remains
and dead shells were formed in great part by the scour of deep-
sea currents out of the upper beds of the lower division of the Coral-
line Crag. At the same time, the perfect state of the Alveolarie and
Fascicularie and the known habits of most of the Bryozoa render it
perfectly possible that many of the individuals may have lived among
these shifting currents and shell-banks.
Crustacea.—Besides the specimen referred to Gonoplax angulata,
Mr. Woodward has ascertained the existence in the Coralline Crag
of the following species :—Cancer pagurus, Carcinus menas, Maia
squinado, and Portunus puber and depurator.
Entomostraca.—Mr. Rupert Jones describes 18 species of Ento-
mostraca from the Coralline Crag*, 3 only of which are known for
certain as living forms (Cythere punctata, C. ceratopora, and Lowo-
concha tamarindus), all in the Atlantic—though Cythere laqueata, C.
sublacunosa, C. trachypora, and C. retifastigata have almost undistin-
guishable allies in the Norwegian sea; and the subdeltoidal Bairdia
of the Crag has its closest analogue (B. fusca, Brady) in the Austra-
lian seas. The last-mentioned seems to be of deep-water habits ;
but the others are mostly littoral.
As we do not know the exact distribution of the Entomostraca in
the Coralline Crag, we cannot speak of them in relation to the dif-
ferent zones.
Cirripedes.—Mr. Darwin has described 10 species in the Coralline
Crag, 4 of which are from Ramsholt and 6 from Sutton. The pro-
portion of recent to extinct species is 6 to 4. Of these six, four are
species still living in the British seas, one ranging to the Scandi-
navian coast and one to the Arctic seas. Both these species, how-
* These conclusions are drawn from Prof. Rupert Jones’s revision of these
Tertiary Entomostraca in 1870 (Geol. Mag. vol. vii. pp. 155-159).
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 131
ever, have an equally wide range in a southern direction, and
the other 4 are entirely southern in their range. Owing to the way
in which so many Cirripedes attach themselves to floating seaweed,
wood, shells, Crustacea, and Bryozoa, their range is generally wide,
and they have less definite value in a geological point of view. Mr.
Darwin states that Pyrgoma anglica is found from 12 to 45 fathoms,
and the Verruca Stromia at all depths from low water to 90
fathoms.
Corals——M. Milne-Edwards could only recognize 3 species of
Corals in the Coralline Crag, and considered them all to be extinct
species,—one, the Cryptangia Woodii of the lower Crag zones, belong-
ing to an extinct genus. Professor Duncan, however, informs me
that in the last expedition of H.M. ship ‘ Porcupine,’ specimens of
a Coral were found alive in Tangier Bay, which could only be re-
garded as a variety of the Sphenotrochus intermedius described by Von
Minster. The habitat of that species is between 60 and 300 feet.
Professor Duncan algo says that the deep-sea dredgings off the south-
west coast of Spain in the same expedition of the ‘ Porcupine’
have yielded a Flabellum which, although not very closely allied to
the Crag form (fF. Woodii), is found in the Miocene deposits of the
south of Spain. This species exists on the sea-bed at a depth of
from 1824 to 5964 feet, and therefore it is reasonable to assert that
Flabellum Woodii was a deep-sea form. It is more closely allied
to Indian species than to those of more northern seas, viz. Flabellum
laciniatum, Ed. & H., and Flabellum MacAndrewi, Ed. & H. Prof.
Duncan further remarks that these genera are such as chiefly inhabit
deep water, and that neither they nor their congeners have ever
formed part of the assemblage which produces recfs.
Echinodermata.—l6 species have been found in the Coralline
Crag, of which only 3 are recent species—2 British and Scandina-
vian, and 1 Mediterranean. If we were to judge by genera alone,
several of the Crag genera are such as are now found only in warm
and tropical seas. Their range of depth is variable. The Comatule
generally inhabit deepish water. Different species of Kchini seem
to mark the different zones of the Crag.
Foraminifera.—One hundred and five species (including notable
varieties) have been recorded* by Messrs. Rupert Jones, W. K.
Parker, and H. B. Brady. Of these, 5 possibly are derived from
other strata; 53 are living species, and 47 are extinct. Of the
recent species, 37 are stated by the authors to be living in the
North Atlantic and 37 in the Arctic seas. The species of the
Foraminifera from one bed of Crag at Sutton, they observe, “ are
remarkable, for the most part, for size and abundance. The
leading forms are Miliola, Lagena, Nodosarina, Polymorphina, Tex-
tularia, Planorbulina, Pulvinulina, and Nonionina. As a fauna,
they are best represented (in our collections) by dredgings from the
Atlantic, south of the Scilly Isles, at from 50 to 70 fathoms, and
from the Mediterranean north of Sicily at 21 fathoms. From all
* “Monogr. Foram. Crag” (Pal. Soc.), part 1, 1866; and ‘Monogr. Poly-
morphina” (Linn. Soc.), 1870. 5
K
132 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
other parts of the Lowest or White Crag of Suffolk, as far as our col-
lections serve, we have got a somewhat similar fauna, not only
greatly reduced in number of individuals and variety of form, but
composed of dwarfs in contrast with those of Sutton, except in
the case of some of those that inhabit shallow water, as Hotalia
Beccaru and Polystomella crispa, and even these are but feeble.
Hence we may suppose that the Foraminiferal deposit at Sutton
was formed either in deeper or in warmer water than other por-
tions of the Crag were. Some of our sources of these less luxuriant
growths are specimens of Crag full of Cyprina and Cardita; and as
the former shells live in the British seas at from 5 to 80 fathoms, a
depth similar to that affected by the Atlantic and Mediterranean
groups of Foraminifera above alluded to, we must suppose that some
deteriorating influence, either cold currents, floating ice, or cold cli-
mate, was at work locally, at least, in the Crag, excepting possibly
the Sutton area.”
Fish-remains.—A sea like that of the Coralline Crag doubtless
contained its due proportion of fishes. Their remains neverthe-
less are scarce. This canin part be accounted for by the fact that
a proportion of them were probably cartilaginous fishes. Small
vertebree of fishes and otoliths are not so scarce. The subject, how-
ever, has received little attention, and requires further investigation.
Mr. Higgins states that all the Crag otoliths which have passed
through his hands belong to Gadoid fishes. The species which
he has been able to recognize are :—
(Morrhua.) | Common Cod.
ms Green Cod. probably identical.
ui Power Cod.
(Merlangus.) Pollack. 1
a Whiting. nearly allied, but not identical.
5 Whiting-pout.
Large teeth of the extraneous Carcharodon megalodon with those
of Otodus, and remains of Platax Woodwardi, of Raia antiqua, and
Zygobatis Woodwardi are common in this as they are in the Red
Crag.
Mammalian Remains.—The term “ Mammaliferous Crag ” was
especially applied to the Norwich Crag by Mr. Charlesworth, to in-
dicate the common occurrence of mammalian remains in that Crag,
in contradistinction to their scarcity in the Crags of Suffolk. The
extensive workings of the Red Crag have since shown that it also is
rich in such remains; but they present this difference from the fos-
sils of the Norwich Crag, that whilst the latter are in greater part
or in whole those of animals living at the time of the Norwich Crag,
those found in the Red Crag are, on the contrary, in great part, if
not altogether, those of animals which lived at previous times and
are derived from older strata. Of this we shall have to speak more
fully when on the subject of the Red Crag. Whilst, however, these
two Crags were known to contain mammalian remains, no land Mam-
malia were known in the Coralline Crag. A few remains of Cetaceans
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 133
had been found, but nothing else. But here again, as with the Red
Crag, the cause of their non-discovery appears to have been that they
are confined almost entirely to the basement-bed of both deposits, and
this bed, in the Coralline Crag, as-well as in the Red Crag, proves to
consist chiefly of water-worn fragments and pebbles derived from
older deposits. It was only at one small pit, and there for a short
time, that the bed of phosphatic nodules at the base of the Coralline
Crag was worked; and yet there were there found as many, or more,
specimens than are usually found in Red-Crag workings of the same
extent. ‘he following species have been found :—WMastodon ar-
vernensis, Ehinoceros (Schleiermacheri?), Cervus, Belemnoziphius,
Balena.
The large teeth of Carcharodon, the skull-bones of Belemnoziphius
and the flat Cetacean bones are all drilled. superficially by some
boring animal. ‘This must, in all probability, have been done be-
fore the bones were fossilized ; and as the holes present mere seg-
ments of their original forms, either they may have been rolled
and worn so as to reduce the thickness of the bone and so remove
a portion of the drilled surface, as has been suggested, or else the
bones may have been originally imbedded in some clays or marls
through which boring shells may have drilled until, coming into con-
tact with the harder bone, they merely impinged on its surface, which
they failed to penetrate. Neither explanation, however, is satis-
factory. In the one case, the bones have generally lost little or
nothing of their substance, while the difficulty on the latter suppo-
sition is that many of these bones are drilled on all sides; one of the
skulls of the Belemnoziphius, for example, shows traces of these
holes on all its four surfaces, whereas, if the bone had been im-
bedded in clay or marl, we should have looked for perforations in
one surface only.
The condition, in fact, of the bones at the base of this Crag is
precisely of the same character as that. of those at the base of the Red
Crag. In both they are worn and mineralized. At the same time
I think it not improbable that the Mastodon and the Rhinoceros
may have lived at the Coralline-Crag period—though the general
absence of all bones other than teeth, and the circumstance that
the materials of the bed in which they occurred is so largely deri-
vative, throw doubt on the whole collection generally. The Whale
certainly lived at that period. The condition of many of the ver-
tebre, their distribution. at various levels, and the occurrence, in
one case, of seven vertebre in connexion, show that this animal
lived in the Coralline-Crag sea, as did probably some of the other
Cetaceans.
From the preceding particulars of the fauna of the Coralline Crag,
it would seem that the differences in the proportions of recent to
extinct species in the different classes is so great that I do not see
how the results are at present to be reconciled. As with the Mol-
lusea, however, I think it extremely probable that the other groups
will, after we know more of their distribution in the greater depths
of the Atlantic, be found to require considerable revision. In the
134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
annexed table I recapitulate this relation of the fauna of the Coral-
line Crag.
Extinct. | Living. | Total.
3 ( Brachiopoda 1 4 5
Sule@ onehitonabe. ss .prettosecktsnanberconee 23 126 149
= 4 Solenoconchia ee 2 2
ON Gastropodalcere-c-crceecnacesseseee cee 28 132 160
a TEIGIHO) NOISE * Goqdansscodonouaoasqebceusoc es 603 1 1
52 265 317
IB TY OZOA tee sein acces necen teeean eck 65 30 95
Hntomostracave-tassscceseeceeteee esate 15 3 18
IRoramimnniferameseesesseereeeecsseneeene 47 53 100
Coral sro nsec enese ree n ocean 2 1 3
Cimempedesiiaynteseseose seen tmesesacre 4 6 10
Hehinodermata ...........0...e0ce000es 13 3 16
146 96 | 242
General Considerations.
Between the period of the London Clay and that of the Coralline
Crag the area now forming the Eastern Counties seems to have
been dry land. Parts, however, of France and Belgium, together
with parts of the south of England, had continued longer sub-
merged, though successive elevations had brought much land to the
surface during the later Eocene and early Miocene periods. The
sea, however, still occupied the western area of Belgium and Hol-
land. This sea gradually encroached in a westerly direction,
and at the Pliocene period had spread over part of the eastern
counties. As it spread in one direction the land rose in another ;
and at the time of the formation of the Coralline Crag a portion of
the Miocene and older Pliocene area of Belgium and the north-
west of France (as, for example, the top of the chalk hills round
the basin of Boulogne), and probably of Kent (Lenham and other
parts of the North Chalk Downs), had been raised and exposed to the
denuding action of the sea, in which the newer beds were i process
of formation.
As the sea extended northward, and the land rose to the south, the
climate became colder, and we have evidence of ice-action even at
the earliest period of the Coralline Crag ; for I do not see how other-
wise than by transport by ice to account for the large block of por-
phyry before mentioned in the basement-bed at Sutton. It is still
a question whence this block may have been derived. I know
of nothing analogous to it in the rock-specimens from the north of
England and Scotland; whether it came from Scandinavia or the
Ardennes remains to be determined. The Oolitic remains were pro-
bably derived from strata in Central England*. The abundance of
London-clay fossils shows a great local denudation, and possibly also
* Mr. Boyd Dawkins refers the Pliosaurian vertebra to the Oxford or the
Kimmeridge Clay.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 135.
a transport from adjacent Hocene land, while the occurrence of flints
shows the proximity of some Chalk shore.
We have therefore in this basement-bed evidence of the sea
gaining on the land, and of the drifting of ice-carried boulders. As
the land subsided the coarser materials of the basement-bed were
covered up by a bed of comminuted shells. This subsidence conti-
nuing, beds “c” and “d” were deposited in comparatively deep and
tranquil water. These beds are succeeded by the sands ‘‘e,” abound-
ing in Bryozoa, with small Echini, and a number of small bivalves,
indicating apparently the greatest depth of sea (possibly of from 500
to 1000 feet) attained during the Coralline-Crag period. A change
then took place, and a bed of comminuted shells, with occasional
oblique lamination, was spread over this deep-sea bed, indicating
possibly a shallowing of the sea by a reverse movement of ele-
vation, and the setting in of stronger currents with intervals of quiet
deposition. Further elevation, exposing the sea-bed to the action of
tides and currents, led to considerable wear and denudation of the
lower beds and to the heaping up of the remains of Bryozoa and
of Mollusca of beds “f” and ‘“e” in banks over portions of the
sea-bed. Under such conditions the upper division, ‘“‘g,”’ of the
Coralline Crag seems to have been generally formed; at a few places
only do some of the beds seem to have been formed tranquilly. I
know of no more illustrative geological instance of the wearing action
of sea-currents than the reconstruction of the banks of comminuted
Mollusca and Bryozoa which constitute this upper division of the
Coralline Crag.
Bed “h” shows, in the finer state of comminution of the shells
and Bryozoa, that the water probably continued to get shallower ;
and finally a continuance of the same movement of elevation gradu-
ally raised the Coralline Crag above the sea, and exposed it to the
denuding action which has removed so large a portion of it. Then,
or during the Red-Crag period immediately following, the Coralline
Crag was broken up into detached islands and reefs, amongst which
the Red Crag was deposited during a period of slow and small subsi-
dence, as I hope to show in the next part of this paper.
The more southern forms of Mollusca which had migrated thus far
north during the Falunian period and that of the ‘‘ Sables Noirs” of
Belgium are replaced in the Coralline Crag by an assemblage of forms
partly of southern range with others of a northern type. Either a
general lowering of the temperature, or else the setting in over
this area of fresh currents from the north (more probably the
latter, as the Corulline-Crag fauna is not a littoral one), owing to
the continued subsidence of land in that direction, led to the intro-
duction of northern forms of life and the gradual extinction of more
southern forms. Amongst the Mollusca we thus see several northern
forms, as Astarte undata, Glycimeris siliqua, Necera jugosa, Tellina
calcaria, Buccinopsis Daler, Cerithium granosum, Emarginula crassa,
Piliscus commodus, Puncturella Noachina, Tectura fulva, and Tricho-
tropis borealis, amongst the Bryozoa the Retepora Beaniana, and
amongst the Foraminifera the Lagena globosa and L. ornata—all
136 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
forms which are now confined chiefly to the Scandinavian or
Arctic provinces. These appear from the commencement of the
Crag period. Of the exact ratio in which these forms may have
increased during that period we are yet ignorant.
The relation which the Coralline Crag bears to the Crags of Ant-
werp has been the subject of much inquiry. It was first treated in ~
a systematic manner by Sir Charles Lyell, and his conclusions still
generally hold good. The corrected lists and more exact divisions of
the several members of the Antwerp Crag, recently given by Prof. G.
Dewalque, have, however, rendered some modification necessary.
Taking the Belgian beds in descending order, the relation which their
molluscan remains show to those of the Coralline Crag is as under :—
No. of species of No.common tothe Proportion of
Mollusca in the Antwerp beds and Corallime-Crag
Antwerp beds. the Coralline Crag. species.
me Sablesjaunes... 197 ...... VSBo. eked 69 per cent.
SENSE oy) Seblagami 4, US ace. 135) ee ate
Diestien ...... Sables noirs... 228 ...... OS aaa A ea,
This question will be treated more fully in the next part of this
paper, in connexion with the Red Crag.
With the Pliocene beds of Monte Mario the Coralline Crag has 147
Species in common.
P.S. Owing to the great additions made to the number of known
species, and the recognition amongst them of so many Crag species
in the recent deep-sea dredgings, the Council of the Society have
kindly allowed me to bring the lists of fossils up to the present date
(April 1871).
List of the Mollusca found in the Coralline Crag.
This List (alphabetically arranged )is compiled from the Monograph
of Mr. Searles Wood, with the addition of Mr. Davidson’s Brachiopods,
whose references and names of species are given in columns I. and II.
Mr. Jeffreys has, with the assistance of Mr. Bell, made some addi-
tions to the list of species; these have the letter J prefixed to them
in column I. The names to which af is prefixed denote species
which Mr. Jeffreys identifies with those now living, in addition to
all the species which had been already recognized by Mr. ‘Wood to be
living *. Every form regarded by Mr. Jeffreys as a variety ranges
through all the columns in italics.
Column IIT. comprises the names adopted by Mr. Jeffreys, except
those to which a { is prefixed, which he regards as synonyms, or
names of later date, but desirable to notice. In this column also
are added other names adopted by M. Nyst for the Belgian Crags;
the last are within brackets.
Columns IV. and V. indicate the zones of depth or bathymetrical
range, and the geographical distribution, both of which have been
furnished by Mr. Jeffreys.
* A very few species, to the names af his a + is prefixed, are not the spe-
cies to which Mr. Wood referred the Crag fossils, although the latter are living.
These are Bulla Lajonkaireana, Eulima subulata, Odostomia truncatula, Rissoa
costulata, and Trophon gracile.—J. G. J.
PRESTWICH —CRAG-BEDS OF SUFFOLK AND NORFOLK.
137
The list of Coralline-Crag localities in column VI. has been
eularged by the author.
The recent work of M. Dewalque (Descrip-
tion Géologique de la Belgique, 1868), which gives the latest lists
of fossils by M. Nyst, has served the author more fully to correlate
the Coralline Crag with the Crags of Antwerp: see column VII.
In column VIII., the correlation of the Coralline-Crag Mollusca
with those which occur in the typical Pliocene deposit of Monte
Mario, near Rome, is given on the authority of Mr. Jeffreys.
Note. Abbreviations:—Lt, Littoral; L, Laminarian; ©, Coralline; D, Deep-
sea; D, depths exceeding 1200 feet.
B, British; S, Scandinavian; A, Arctic;
M, Mediterranean ; W, West European; At, Mid-Atlantic; Am, North America ;
A, Aldborough ; I, Iken; Sd, Sudbourne; G, Gedgrave ; 8, Sutton ; R, Ramsholt ;
Go, Gomer; B, Broomhill.
I. Bracwropopa.
if We iit VEE VE WE WO | | ASU
=I Localities) Beli | Ttay.
Ba N £ Speci Critical remarks ae Geographical | in the ne =
os Sa Sa? eae and synonyms. cee distribution. |Coralline} = | 2 4}|Monte
BD So Ras Crag. |3.4| 3 3 |Mario.
Ais Nw!) 0S
10. | Argiope cistellula ...; Orthis lunifera, Phi-| C BSM Ss)
lippt?
5. | tLingula Dumortieri 4] L. jaspidea, A. C Japan SB | %
: Adams.
7.| fOrbiculalamellosa?, Discina atlantica, At N}
King.
16.| Terebratula grandis 4 T.ampulla,Brocchi| ...... | .........0e SSdBGol x | x *
12. | Terebratulina caput-| Genus Terebratula..| L-D |BSAMWaAt) §S
serpentis.
II. Concuirsra.
evhe| Abra alba, v.50 0250s Genus Scrobicularia.| Lt--D|BSMWAt §S ox| ¥ *
239. prismatica...... - ¥, L-D|} BSMW S Go jox]| x *
9.| Anomia aculeata ...| A. ephippium, var....| 0000. | ..-.eeeeee Sgt askioda| Weanae
8. Gyo OMT Gad] eadoconndooccee Lt-D| BSMW | passim Jox | x *
10. Pate llttormisees|e vases eters = RB SeAGMOW. |) USdS Peeeai|tee.-- *
ine SCMAUG 0.0.00. Zale FETA OPTLOS OOTS| Gaccon ||| aeebocooceee passim | * | *
(QICIPATCANIACHCAN SS. cocccveiiir= | eesseeceaaces L-C | BM W At Ss Ors, [ bens *
79. pectunculoides}(A. pusilla) ......... C-D|; BSAM Go |) © besese *
76 (STEEN? Saasee|| le aeoabncaneoccen Lt-D |BS M W At SdSR}.....)...... *
215.| Artemis lentiformis | Venus exoleta, Zinné,| Lt-C} BS M W G? x | x *
var. (Dosinia exo-
leta).
215 sun chaie ee esee se G. Venus (D. lincta)| Lt--D|} BS MW SR x | x *
177.| Astarte Basterotii ...| A. suleata, Da Costa,| L-D |BSAMW At passim | * | x *
var. |
22a! Tg TPR ge crn ncec odd beep] (a ee a passim | * | x
190 digitaria ...... GaNViooditanee este: CD; BMW SGo | x | x
Re ACXENTECNS)25. 03" 1) ureter IRR a! a eeccceccons Sas aa lal be tecs
* T have further shown by the mark o in the column with the “Sables gris ”
those shells which are found in the ‘‘Sables noirs” of Antwerp and Hdeghem.
138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
ConcHIFERA (continued).
L II. Til. VE Vv. VI. VII. {| VIII.
A aS Critical remarks AOR: Geographical ee ‘Gage a
Se : ritical rem ee
2 ISIE Gi opps ues and synonyms. | q epth distribution. |Coralline} 2 | 22 bie
&9 : ag. |i .4 | § |Mario.
dg me BE\aE
185.) Astarte gracilis ...... A. compressa, Mont-| C BS AW | passim] x | x
agu.
186 UNCETTA ..00-- 000 A, pica BU sel] cooaes || sopeqos00302 gs x | *
178 INCTASSATA .....- wily SURO, CLIP, sonencl| coonco | aqanceoacene Sd Viens *
179. —— mutabilis ...... Italian Pliocene ...| ....2. | s.ecseeeeees assim jo x| *
180.| t— Omalii ......... qA. undata, Gould | C Am SGRBGo} x | x
192.| -—— parva............ A. pusilla, Forbes ...| C-D MW S:Go. Fon lees
175 parvula.........| A. triangularis, var.| C At EDN bepecalacacac
187.) —— pygmea ...... CGS Walia) cacasneds|), ede009 |] _coonaannacee SIP ti becuse iaccioce
173 friamManlarigysc|eo = leeena aeeeaee ee L-D | BMW At | SGo | o |......
51.) Avicula tarentina ...| A. hirundo, Z. ...... L-C | BM W At Cae bis. ccl boades
167.) Carditachameformis| C, scalaris, VOT. ...00.| seecee | cececeeecees sd s x | *
168 CORDISN eseoeat eli) percemeceieeneeek on Cc M W SBGo] o |......
167 OHOTEMIETI Saco) |. Boocdagcaduagae: |, booues IP adoadecdooos SdSBGolox| x
166 GHENT Badpbnosoll beni) odeecdaosAedoe) | \||/oceanahl| caedssoudodd Sd GSB] x | x
Go
165.) t— senilis ......... C. suleata, Bruguiére| C M W passim ]......|......
159.| |Cardium decortica-| C. levigatum, Poli...| C MW passim ]......|......
tum.
155.) —— edule, var. rus-| —............4.8- Lt-L| BSMW R * | *
ticum.
153. nodosum ...... C. fasciatum, Mont.) L-D |BS M W At} SGo } o |......
J |f— norvegicum, | —........-seeeee L-D |BSMW At) ....... * *
Spengler.
154.| t— strigilliferum | C.elegantulum, Mol-| C A S BiGonene ee
ler.
162.) Chama gryphoides...) —.............-- Lt-C MW So ob aval
198.| Circe minima.........] 9... sseeeeeeeees L-D |BSM W At} SGo | x | x
264.) +Cochlodesmapreete-| Thracia prztenuis,| Lt-D| BS M W 8c eee
nerum. Pulteney.
200)\(@oralliophagakeypori-| sale cepecesacece cine |iccee inl Mirae sere eee SER ieee x
noides.
274.) Corbula striata ...... C. gibba, Olivi ...... Lt-D|BS M W At! passim Jox] x
135.) Cryptodon ferrugi- |G. Axinus ............ C-D|BSAMW S (>) ibogeeelieean
nosum.
134 sinuosum ...... A. flexuosus (Lucina} L-D |BSAMW At} SGo jox)......
sinuosa).
258; Cultellus;teniisi veau |i) py ween sdcedesees soe 0h t]| dace) Misteeacerisees: S : fea *
Uo w(Cyenmrivarely Grshreuntte Vs skesscsigncase || cescce || Sdorescnuese SI ee 2 er
196.) Cyprina islandica...| —............++ Lt-D BSW passim }ox] *
197. SADTINYEC) goesoaeal|) Wi aceacodancoodecon! || “eoodan il" Gabscounseer SdG@Rlox| x
B Go
207.| Cytherea chione...... G. Venus (C. cypri-| L-C | B M W At RB Jox] x
noides).
208.) —— rudis............ G. Venus (V. cycla-| C MW passim |*o| *
diformis).
146.| ¢Diplodonta? astar-| D. trigonula, Bronn| C-D M At s x | *
tea.
145 dilatata ......... Dirorundata,var(D:\ sn... |) seseeeeeenes Ss go = | becom
Woodz).
144.) —— rotundata <0...) .cceeeceee ee L-C | BM W At | passim |......)......
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 139
ConcuiFera (continued).
i iT III. IV. Vv. Wal
S 3 Zones | ¢ — pee
oe : Critical remarks eographical} in the
® = Bea oF ene: and synonyms. | 4 on distribution. |Coralline
Sp Sp epth. Crag
As
220.| Donax politus ...... (D. vinacea) ....... .| Lt-C}| BMW |GS8Go
171.| Hrycinella ovalist? | .e..sseecceenee | sereee | ceetessen ees GS Go
217.| +Gastrana laminosa | (Fragilia laminosa) | ...... South Africa GS R Gol *
292.) Gastrochena dubia | ——.....-....---+- L-D | BM W At S)
291.| Glycimeris angusta | Gl. siliqua, Chemnitz| L-C BK Se ie R
0)
19.| +Hinnites Cortesyi ..| H. giganteus, P. Car-| ...... Am R
penter.
150.| +Hippagus verticor-| H. acuticostatus, C-D | W At Japan 8
dius. Ph. ; G.Pecchioiia,
Meneghint.
193.| Tsocardia Cor ....00...| seeeeeeeeese eee L-D} BSMW | GSR
120. +Kellia ambigua ...| Erycina pusilla, Ph.| C BM S Go
123.| -—— coarctata ...... Galeomma compres-| C M Ss
sum, Ph.
122.| -— cycladia......... G. Axinus; not Scac-| C—D BM 8
chia ovata, Ph.
121 elliptica.........|G. Scacchia ......... C-D M At Ss
120.| —— orbicularis...... A. CYCLAAIUS, VAT. woe) verre | senseeeecees s
124.) -—— pumila .........] _seereeceeeeneee D B At Ss
125, TUVONID nsoocn0608 G. Lasea ............ Lt-C |BS M W At Ss
118. suborbicularis | —...--- +22 e+ Lt-D |B S M WAt Ss
95.| Leda pygmea ......] 0 eeeeeeeeeeee eee C-D |BSAMWAt|GS RGo
91.) —— semistriata ...] .cescecesoeeeee | ceeree | eeeeeseeeeee SRB
115.| ¢Lepton deltoideum| Erycina Geoffroyi, | © M SR
Payraudeau.
|t—-depressum ...| L. nitidum, Turton | C BM W 8
.| —— nitidum:........ L, squamosum, Jum. | v1.10. | ceseeeeeeees s
} SQUAMOSUM ...] — seneeeeeeeeeees L-C BSW 8
fLimaelliptica,Jeffr.| — ..ssesseeeeeeee C-D BSM S
.| T—— exilis ............ L. inflata, Lamarck M R Go
MEHR! seobsacod var. tenera ............ Lt-C |BSM W At R
—— Loscombii....... .s--ee.--s-eeee L-D| BSMW | SRB
.| —— ovata ......20008. Ostreanivea, Bre. ...) 0.0. | ...s0-c.eee- S
.|t—— plicatula ...... L. squamosa, Lam...| C M S
| —— subauriculata | Certainly Montagu’s|) C-D| BS AM W|SRGo
species. At
.| + Limopsis aurita ...| (L. sublevigata) ...| D-D |B A M W At| G BGo
| t— pygmea ......| (LL. anomala) ......... C-D MW S Go
.| Lucina borealis ......) «-+2--2+-2+- ++ Lt-D BS M W At} passim
|) Ss ORME, Coca] | Gaonesopcdoogo ||| aa99e5 || saagasccos6e SB
GCC sesncdl| | ccannsoeccgueca = ||| waccse | sagscsaa000 S
| Lucinopsis Lajon- | esseeeseeeeeeee C M SR Go
kairii.
.| Lutraria elliptica .... .cecsseeeeeeoes It-L| BSMW /|SdRGo
oblonga, (Chi...|) -serecnser sao Lt-L IBUMEGW lire.
.| Macha strigillata ...) G. Solecurtus......... Cc M W iS)
.| Mactra arcuata ...... M. glauca, var. ...... Lt-L| BMW GSB
OTLOPUD ... 2.2006 LL, GUARERD,; WPS o330e)| secpps |||) gacdeoas60 sd
.| —— obtruncata...... M. subtrumcata, var.) .......| 2.-.2.-+0--- $ go
+ Miocene, North America (Conrad).
140
ConcuirerA (continued).
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
.| Nucinella miliaris...
.| Nucula leevigata
.| —— nucleus .........
tenuis .........
t—- trigonula ......
+Ostrea cochlear, Poli
J | +—cristata, Born..
13.| —— edulis............
17. princeps ......
270.) Pandora inzquival-
vis.
283.) Panopea Faujasii ...
29.) Pecten Bruet ......0..
38.| —— dubius .........
24.| +—— Gerardii ......
22.) —— maximus ......
30. opercularis
31.) +— princeps ......
23.] —— PUSIO ...000......
25. —— similis ......
27. tigrinus.........
66.) Pectunculus glycy-
meris.
.| Pholadidea papyra-
cea.
I. II. Iii.
}
ane Critical ks
‘o'&| Names of Species. a ae Tenure
28 and synonyms.
Ie)
AY Ss
246.) Mactra ovalis......... M. solida, Z., var.
elliptica.
Ail |) ———— SSAINOEWOE Goons] gnvepecconocoon
325.] t— triangulata ...| M. subtruncata, Da
a.
60.| Modiola costulata ...)G@. Modiolaria ......
62.) —— marmorata ... ; sc ieee secs
57.| ——modiolus ...... G. Mytilus............
8); ———— JOR eOMM cod! pg gp caabaoccoun:
64.| —— rhombea ...... G. Crenella (C. Pri-
deauxana).
61.) —— sevicea ......... (@Nsericea) #0. fnese:
J |tModioclaria discors,) ..........-....
126.) Montacuta bidentata) —................
NEN 4p —— 2 ClomeVeE oooell | oogasasasonoc06
129 HEFTAVISONOKE, aacl|—canqagooenodece
128 substriatanssten. ety acne:
127 EVPUNCATA soeeee M. bidentata, var....
PAT o)| WY. (TRUDE scedooscs| | gcevqoueaaccecd
55.| Mytilus hesperianus| M. edulis, Z., var. un-
gulata.
273.| Nera cuspidata ...) .........0..00-
272.) —— jugosa ......... qN. lamellosa, Sars.
(N. ovalis)
wesc ese eeOtece
wee e ee cect cence
Waell).
eccccccccces 808
ee ecesececeeeie
eer ecesooccecee
Coc cccceccescce
soccer coeees
P. dubius, jun.; not
Brueit.
SOOO
Cre ccrccccccsce
wee cee cecececee
ees ercoesescce
eae een eee reesce
et accceeeooccce
Cece re te 20eccvce
eoccee
eoeeee
We
Geographical
distribution.
woccecoescce
eee veoeecece
i
43 245
edited
o
ea)
i
cs
4
VI.
Localities
G? Go
passim
Sd SR |
Sd G R }
passim |
passim |
passim
passim.
S Go
passim
passim |
Ss
Jn oe eee
eoneee
seeeee
eoseee
eeceee
eeceee
VII. {| VIII.
Belgian.
Crags. | italy.
PRESTW1CH——CRAG-BEDS OF SUFFOLK AND NORFOLK.
ConcuiFera (continued).
141
I. II. Ii. IV. We VI. VIL.
2 Localities} Belsian-
a8 N £ Spec} Critical remarks meee Geographical | in the ie
28 ames Ol species. and synonyms. ean distribution. |Coralline} g | 22
zp & ia Crag. |2.2/2 5
uu ¢ AD | 7S
MoiebaladomyaGesterial) —....,cc<scrpsense «| \e=<en su, )irnskneepeo ae Sd R Go?l....-.|-0000.
296.) Pholas crispata ...... A fragment only Lt BSW SS) | kesocd|ooasine
295. GyyliTRG RE SsanBat tes Gragereaenesd ale Il Sacred. IWietoteedasdacts Sie) | Bacandlaccco:
00.| Pinna pectinata (?)| P. rudis, Z. ......... It-D| BMW At | passim Jox| x
268.|Poromya granulata; — .........s0e.e C-D;iIBSMWAt! GSR Jox.|......
J |tPsammobia costu-| ............e0s JOpID) 1B) 1S) WE VV NG) egceen | Rosoce||bscbec
; lata.
222, Ferroensis...... L-D |BSMWAt/GSRB] * | x
223, nellitaveles scn65q) © sagocdeqnnca5ec L-D BSW Sian) | Rested eoeene
222 vespertina...... dpactcosnbeeods It-C|BSMWaAt| SdR l...... *
Ben-Saxccava arctica ...| S.1Uugosa, Var: ...0..| sovey. | cececeeeeeee s ox} ¥
289 ? carinata ...... Jeena, JWOCCH, || gaaoca' || cornance svar GWGIO | Leese dete
Mont., var.
288.) +— ? fragilis ...... Ie plicaitaneessscencers L-D BSW Ss o | x
285 GUT ORE wre SAB Seay (ROLE ISS cae eden It-D/BSAMWAt SS Oil seaie:
J |+tSolecurtus antiqua-| —.............4. TEC WBS WAG 0 occ shee %
tus, Pult.
BI SOLENENSIS 2... ccccca:|) dan scacesccessen L-C | BSMW | passim Jox| x
276.| Sphenia Binghami? |G. Mya ...........08 L-C BMW IS} 14] basasulsaocoe
203.| Tapes perovalis ...... Le CURTURGUS, Ibe, GER ccoiven || \ adoonanddoac PN beaobe *
201 VIFgGinea......00+ a a Lt-D| BSM W Ss frees (hoe
227.| Tellina balaustina ...| .....s.ssseeeee L-D | BM W At Ss a || 28
226 GDP Scagescaded| |), acbonacansadooe Lt-D| BSMW s x | x
234.) +—— donacilla ...... T. compressa, Bre... MW S Se ealfsie:
233 GO DREIND, “sgoocal| _ » saeboooadacHanHo L-C | BM W At SdSBGoj « | x
228 obliqua .........| T. calcaria, Ch., var.| L-D| B? S A At SdRBGo) « | x
300.| Teredo norvegica ...) ss. .seeeseeeee Lt BSM W SR x | *
J |TWhracia distorta, | ....csces..ceee Lt-C| BS MW Sd x | *
Mont.
Polelp=———aintatan .ccccecs T. corbuloides, Des-| C M Sd B Gol...... *
hayes, var.
260.| —— phaseolina...... T. papyracea, Poli... Lt-D |BS MWAt| SGo | * | *
259.) —— pubescens ......] see .eseaeeeeeee C-D| BMWAt| GS |...... *
262.) +—— ventricosa...... T. convexa, W.Wood|) L-D| BSMW | GBB }...... *
ZLOh Viens CABIUA, 5 J....10<0| ¢ Plesanecennescoes L-D |BS M W At} passim | * | x
212. imbricata ....../ V.fasciata, Da C., var.) Lt-D |BSMWJapan|G R BGol......|......
213. OVEN spgnbocanda| = =o eSassesenonnebo0 L-D|BS MW At} passim | x | x
IIT. Sonrnoconcata.
190 |+Dentalium bifissum} Dischides Olivi, C-D M W SiGoweSeece|besee
Scacchi.
188.) —— costatum ...... DFdentaliswi., casa C-D M W SLGOMe Ore ltesene
IV. Gastropopa.
J |tAclis ascaris, Turd.) —-... ss eeeevaee C-D | BSMW Sei iccceelliaceoee
J |t— Gulsone,Clark| —....-..0..000-s C BW Sie oilesscee senses
o | t— Walleri, Jer.) oo... ec eceeesee D-D|BSAMWAt §S Bets
171.| Actzon levidensis ...| (Tornatellaelongata)) ...... | .........-+- iS) Oust e sees
170. hornaiilisheccc\ — cusemeeecaces D| BSMW Ss @) € |badber
re
Page of Mo-
nograph.
.| Alyania ascaris
.| -—— nana
.| --— ventrosa
.| Ceecum glabrum
.| —— militaris
.| t— cribrarium
.| -— granosum
| T—- metaxa (?)
142
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Gastroropa (continued).
II.
Names of Species.
.| Adeorbis pul chralis
.| t—— striatus
subearinatus ...
.| -—— supranitidus...
tricarinatus ..
.. Aporrhais pes pele-
cani.
.| Buecinum Dalei......
undatum ......
Bulla acuminata
concinna
—— conulus
ecceneees
—— cylindracea ...
+—— Lajonkaireana
oeaccceae
truncata
ecotee
| Bulleea quadrata ...]
scabra
sculpta
woceeren.
incurvatum ...
+-— mammillatum
trachea
Calyptreea chinensis
.| Cancellaria costelli-
fera
.| -— mitreeformis (?)
scalaroides
-| T—— subangulosa ...
.| ¢Capulus fallax
aenees
—— ungaricus
.| t2?Cassidaria bicate-
nata
.| Cerithium adversum
.| A. supranitidus, var.
q{C. Macandrei, Z.
III.
Critical remarks
and synonyms.
Babee b new bereene
Trochus Duminyi,
Requien.
Aclis supranitida, S.
Wood; not A. as-
caris, Zurt.
G. Cylichna
Not B.conulus, Lam.
C.umbilicata, Mont,
var.
G. Cylichna
Utriculus obtusus,
Mont., var.
G. Scaphander
G. Utriculus
U. truncatulus, Brg.
G. Philine
notC. trachea, Mont
Admete viridula,
Fabricius.
C. varicosa, Bre.
Piliseus commodus,
Middendorff
C. ungaricus, jun....
C. ungaricus, LZ. ...
C. tyrrhena, Ch.,
var. ?
G. Triforis; T. per-
versa,
Adams (not C.
sinistrorsum, JV.).
Cerithiopsis metaxa
eeecee
Vy.
Geographical
distribution.
eer tees ances
a
.| t—— concinnata
.| —— retusa
.| Erato leevis
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK.
GAsTROPODA (continued).
143
II.
3
S &) Names of Species.
Ss
As
72; Cerithium perpul-
chrum.
70. trilineatum ...
70. tuberculare
80.| tChemnitzia costaria
79.| -— curvicostata ...
82 densecostata ...
81 elegantissima
82:| —— filosa ..........:-
81.| -— internodula ...
80.| -—— nitidissima (?).
79 MULL BN eat cliches os
84.| —— similis .........
83.) —— unica(?) ......
84,| -— varicula.........
185.| Chiton fascicularis(?)
Rissoi (?)
eecoee
.| t— strigillatus ...
Clavatula brachy-
stoma.
cancellata
aevcee
castanea(?) ...
costata(?)......
.| —— levigata(?) ...
.| —— linearis
.| —— mitrula
perpulchra......
— Philberti
.| Columbella sulcata ..
.| Cyprea affinis
avellana.........
europa
tDefrancia hystrix,
Bellardt.
.| Emarginula crassa...
t— elongata, Costa
fissura
+—— rosea
Maugeriz
.| TEulima glabella .
...| G. Cerithiopsis
...| P. decussata, Ph. ...
I.
Critical remarks
and synonyms.
Cee cece eseseace
G. Odostomia
O. indistincta, Mont.
O. rufa, Ph., var. ...
O. lactea, Z. .........
G. Odostomia
§1C. Corbis, Conti...
Not O. nitidissima,
Mont., but allied
to O. acicula.
A doubtful identi-
fication.
O. filosa, Var........+.
Not Cioniscus uni-
cus, Mont.
G. Cerithium
C. cinereus, ZL. ......
C. Hanleyi, Bean ...
Pleurotoma concin-
naa, var.
Defrancia reticulata,
Renier, var.formosa
D. linearis, var.......
G. Pleurotoma ......
” ”
G. Defrancia
P. costata, var. (not
P. mitrula).
D. linearis, var.
equalis.
Defrancia purpurea,
Mont., var.
COU gnngnn ii iit
OOO iy
wees ese oe ces vee
Cesc erccccccsece
Possess sccsee
.| —— polita
VE Vv. VI. VII.
Localities] Belgian
4008S Geographical | in the seats
deoth,| ‘istribution. |Coralline| g_ | 2 ¢
se Crag. [32/38
DH | M.S,
Saeed Gere
Cc Si Gow es ok:
Lt-D|BSMW4At]| SGo J......)......
C M Siete ee ee
Lt-D |B S M W At Siete | Reeee eine
eer life tance nate s Le sebuliesees
Lt-C|BSMW At| SGo |......)......
Seicistevey ul) ir Sine Wer S peta an lees
C-D M W Sine RRs *
D M S eucereyaeeade
L-D |BS MW At SHTUEEG tates eee
Sree heh itiss ots cram Ss Opel lian
Pee NS) OF slhetee.
D Ww SSiertiny HeGe esol peice
Lt-D |BS M W At Sie eon Badaas) oar
ItD|\BSAM W Sele elieeell geckd
C-D BSM Sr Gules:
Esk lsicce lm ends tanec 8 Pella ae
L-D| BSMW | SGo |.........0.
ess cell tea Rate tarsal 8 go wslMaweer
C-D M W GS Gol......|......
It-D| BS MW SGo ]...... *
Lt-C | BMW At Siete bee lige
L-D|BSM W At Shales seul ecee
satire si cea SEGON) [hcwsee| saves
He Sca Aer eee ae SuGfO) ASSN caer
Lt-D/IBSM W At NS)
heel aie cee aber ace 2 NS) Bebe ua|ib. Se
rR ROEAI) Wha AE ESS Ss CS Ait ae
Pee tnoe ||enenc Sit eat S aise aaa
LtD| BSMW |SBGofox|] x
SAMA Mee cheep taee S) Gio) | basonclosncee
C-D M S Sepals a
Lt-D BS W SRGo]} x | x*
C M Shah eal (oneere hataesc
It-D|BSMW At} SBGoJlox] x
L-D BM W SON ae Behan
I-D BM W S Go Op eeean
C | West Indies | S Go J}......]......
C-D MW SSIRMeege | (aeaieese Las sae
L-D | BSMW Sic baessibbae
I. II. Kil. Ve
8
= re one Zones
‘S =! Names of Species. eet veiealis of
2 5 and synonyms. | denth
SO
Ais
97.| fEulima subulata...| Not E. subulata, | D
Donovan.
J |fFissurella costaria,| {F. neglecta, Desh...| C
Basterot.
168 Fexgt teh!) aacOOBBGE CU Mudeoouresdeoaee Lt-D
ae Fossarus sulcatus .| (F. clathratus, Ph...) C
319.| Jeffreysia ? patula ...\Velutinavirgata; fry| ....9.
122.) Lacuna reticulata ...|G. Fossarus ...... ..| «.-+..
88.| Litiopa papillosa ...| Qu. G. Litiopa? ...| ......
135.| Margarita (?) macu-| (Solarium turbimo-| ......
lata. ides.)
136 ROO NOC cnoda| | "| ogascaeasodsace | || -onocos
151.| Marsenia tentacu- |Lamellaria perspi- | Lt-D
lata. cua, LD.
J | {Murex aciculatus, |4{M. corallinus, Lt-G
Lam. Se.
40.) t—— tortuosus ...... M. erinaceus, Z., var.) Lt—-C
oO} Miibravelenusiacesehece spies seenacs yee Lt-D
21 plictferd......... M. ebenus, var. ......| ss.
31.) Nassa consociata ...| N. elegans, var....... C-D
29. AE MUUEHID) | cacoc|! Asdanancoacsges C
29. WOCHEISSEMI) Basnooll | sneodscossouoge Lt-D
28.) t—— labiosa ......... N. semistriata, Bre. | C—D
32. prismatica ...| N. limata, Ch. ...... L-C
315.| —— pygmea ...... N. incrassata, var.| ......
simulans.
145.| Natica cirriformis ...| N. sordida, Swains. | L-D
J |t—— heros, Say...... qN. catenoides, Lt
S. Wood.
148.) —— multipunctata | N. millepunctata, Cc
Lam.., var.
143.) -— proxima ...... N. cirriformis, var...| ......
143, VATIANS ......00+ N. cirriformis, var.?| ......
J |+Odostomia acuta, | — ........sces00e L-C
Jeffr.
J |t——inseulpta,Mont.) —........se0eee- L-D
J |t——obliqua, Alder | —— ..eseeeeeeeeeee C
86.) —— pellucida ...... O. decussata, Mont.,| C-—D
var. :
85.) —— plicata ......... O. conoidea, Bre. ;} L-D
not O. plicata,
Mont.
86.| T—— pupa ............ O.interstincta, Mont.,| Lt-C
var.
87. simillima (?)...| Not Turbo similli-| ......
mus, Mont.
318.) t— truncatula...... O. plicata, Mont. ...| L-C
14, Ovula Leathesii...... Bulla spelta, L....... C
109.) Paludestrina ulve...| G. Hydrobia ......... Lt-C
54.) tPleurotoma cari-| (P. modiola) ......... D-D
144
nata.
Gastropopa (continued).
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
We
Geographical
distribution.
SOOIOUO Iie ii
Ri
BSMW At
BSMW At
were ee eeeeee
BS M W At
BS W
BM
BW
BS M W At
BS M W At
atc cere sece
VI. VII. {| VIII.
Localities foe Italy.
in the —_—
Coralline}] z | 2 4}| Monte
Crag. | 3-2| 2 §| Mario
wm &| n.8,
SRGofox] x *
Se | Peon ecli eh *
SRB] x | x *
Po ne oe
Sie ae
Si Govtaeeee eee
Stale
SGo fox] *
S!BiGollvereel seer
8, sola
GS RESss las
Soa *
S'Gojaeeeaeee *
g at
GS Go *%
S Go) [ee *
N) Ox! x *
GGo }ox] x *
G Go Jox]| x Loe
See *
R Go * | ¥ *
Sin ciy/ bee eee
GRGo} x | x *
7 b go }....-.. *
BGO || bococs||scoo5:
SS. chegeeeleee
“8 Calc
N) Opalavan *
GSRGoj o | x %
Sen (a sonn|hsaaad ¢
See Peau Ree
SiGoy Peal aioe
SIGIO. || baeooe *% ¥
CER | ENsanhl Haees.
Geissalieee
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 145
GastRoPoDA (continued).
fi
II. Til. IV. Vv. VI. VIL.
ig | Localities} Belsian
Fa a] ON f Speci Critical remarks fone | Geographical} in the eos
os ames Of species. and synonyms. Aesth distribution. |Coralline Da
a 0 due Crag. ag
4s n.S,
| J |Pleurotoma nebula,) — ............... L-C BMW
Mont.
55.| t-— porrecta ...... P. nivalis, Lovén ?...) D-D IBISAt | (GiGow iol
54.| -—— semicolon ...... P. galerita, Ph. ..... C-D |; BM At HO) Ap EN el Be, 4
et strtolata, 96. .s.| ..cseseceenesee C-D |BSM WAt Soy vie Mf SEB terse
Me Remieri 2. scc| | cscesccernnees D BOs gren Gee te hen Ns see
J |fPuncturella no- Sonemcaae se C-D| BSAW Sp RTA eee
achina, L. |
77.|tPyramidella leevi-| P. uniplicata, Dujar-| D-D MW Grou vay |sezeee
uscula. din (P. plicosa).
49 P. subintermedia, I
311. | Pyrula acclinis Bron, (Ey Leti= ise cas )|! asjoeseaerens R *
: culata).
22.) Ringicula buccinea | R.auriculata,Menard| C-D | MW At s %
22,| T—— ventricosa......| seessesaseeeeee D-D| MW At Soa aed
Pera PESISSOAKCOTMTUSIO 2 F.4|| TR. a2. sttnecce accel iole|| ssuswee soi eeemiarennas S Go peered
106.) t—- costulata ...... R.Stefanisi,Jef?.;n0t| D-D M W poate aaa tend
R. costulata, Alder.
| 106. NARA IA DE ou| 1) Laiekeencacwnnic: Oh alipsasieeay ip luis SRR ERE S Brea tere
REN AM SOUCH ccc ates.|/icnagWeaeesoesgan vy ||yaeeeerdty SUUeRESD owe SiGiony Weasels a,
J |t—proxima, Ald.) oo... seeeee eee CD; BMAt SUL, ee pea
| 103.| t+—— punctura (?)...| R. concinna, Wood ;) 100. | seeeeeeeeeee So Relihonab.cucl
not R.punctura, Mont.
103.} —— reticulata (?)...) R. calathus, Forbes §| L-C | BS M W At Sn] bodaeel daca
Hanley ; not R. re-
| ticulata, Mont.
318.) ——soluta we) ceeeeeeeeeeeeee C-D |BS M W At Siete Geral apee re
100 SUTTER Ha ee Lt-D|BSAMW At S — #-......)......
107. supra-costata...| I2. CONfiNIS, VAT. ....4.) veces | ceceeeceeese ST alee et
102.) —— vitrea............ (Not R. vitrea, V.)..., C-D | BS M W At S *
101 Zevlamoicneesslt | seuteesssceccee L-D |BS M W At Seiya le: auleerhs.
95.) tScalaria cancellata | NotS.cancellata, Bre.) C-D M At SiGor melee
94 Glaplrabuleverts. hy) eieeeeeee cece tc L-D; BSMW |SBGo *
91.| —— fimbriosa ...... S.lamellosa,Bre.,var.| ...006 | vsccecceeees S83) © 63 Inaanodt
93 FOUACED ose n ses SEF RORAOSAN OCT (OS ayes a\i\) istsos tactics 8 go *
frondosa).
92. GroMdiculareccs|on —xteeces era Rall (aR A beaeseeR nena GSGofox| x |
92.| t—— frondosa ......| QS. soluta, Tider’...) D-D| MW SJ et algae oceae
91 hamulifera ...| S. fimbriosa, var. ...| ....++ | sernveeeeren STi BARU leases
29. — obtusicostata... -......-s0..ce0e D-D | At DS itaatiteeamel cpcunes
93. subulata......... SG MOIAREAG, CHIR, casouel): coobee. ||| \\eotmoadeooae sb go Sab ree
90. SUPIGU Oa oo tbo SEN ATAQOSUE, ClURs (Goes|. 66005; |. aniedeenncnee SHISIG OMOEA.
163.|Scissurella crispata | .......s0ee000 DEB SeAw VGVVEN Liam Sin MLE een hen
149.| ¢Sigaretus excavatus| —...secssceeeeee | D W Sp ADE aie
MGHeMectura fulvaccscscces| <0) svevswteccseds CD; BSAW Feira) Beemer semen:
26.| Terebra inversa...... GiColumibellayemece\\ osm: an ll see tees aces GGo t x | «?
26.) —— canalis ....04... GS COTA, OG CHOU! “Shane g ill wegacenceacce cle wodcsee | bocsaa scone
‘ trorsd. |
G7.| Trichotropis borealis)... ..sseesseeee TEST) | apa SGP/ARIS inn <Gho0 Abeea dea
41.| Triton heptagonum) Not Murex heptago-, Lt-C | BM W At, GGo }......|.....
nus, Bre., but T.! i
cutaceus. |
VOL. XXVII,——PART® I, i ; hana
146
GastROPODA (continued).
122.
f a
es
113.
20.
.| t—— ditropis
.| —— formosus
.|—— Kickstt
.| —— Montacuti
.| —— obconicus
.| t—— costiferum
|| T—= gracilius ...
.| —— imperspicuum
.|—— muricatum .
.| t—- paululum ...
II.
Names of Species.
Trochus Adansoni...
— bullatus, Ph....
CONMULUS seccseoee
OOOO Ory
ences
millegranus ...
tricariniferus...
.| —— villicus (?) ......
zizyphinus
.| Trophon alveolatum
consociale
| t—- gracile ..
+Turbo spheroidea .
Turritella incrassata
6.) t-— planispira
tVelutina virgata (?)
+Vermetus intortus .
+?Voluta Lamberti .
III. IV.
Critical remarks fone
and synonyms. | 4 epth.
A doubtful identi-| Lt
fication.
Italian Pliocene ...| ......
T. zizyphinus, L. ...| ...0-
T. biangulatus, Hich-| C
wald, fide Hornes
T. occidentalis, C-D
Mighels, var.
T.Adansoni,S.W.,var.| ......
suaswosuedecats C-D
A doubtful identifi-|) I-D
cation.
T.Adansoni,S.W.,var.| ......
sa@enesesicoeets Lt-D
T. alveolatus .........| ......
T. alveolatus, Var. oo.| ....+.
T. costifer ............ D
Not Fusus Seah C
Da C.; F. curtus, J.
G. Pleurotoma ...... D
T. muricatus ......0.. I-D
Defranciateres, Ford.,| C-D
jun.
Cyclostrema sphzro-| C-D
ideum
T. triplicata, Bre. ...| C-D
1. subangulata, Bre.) C-D
V.undata, Smith ...| D
V.subcancellatus,Biv.| Lt-C
V. Junonia, Ch.?...| D
PROCEEDINGS OF THE GEOLOGICAL SOCTETY.«
Vy. VI. VII. | VIIL.}
Localitiey Belsia> | Ttaly,
Geographical | in the See — |!
distribution. |Coralline| 2 _| g g | Monte
Crag. |-2-2|-3 5 | Mario
nN | 0.S
M S Go * | %
Sac nhase eae Go Useaashlaasee
Prec r *
M S. lbvesslevneet
BS S.B abies *
ist de means 8 go halo. om
BS M W Go Oldlaarag
BM W At Ss nosenolese ace *
sokepicidaes S Go [.....-]...08-
a Tid cetetes Ss Sogstrall ta eae
Lele a ele ree S GO. Neasiea\pancs
BSMWAt|ISRBGo} x |......) ¥
aaigaaaaaeaiee G Go * | x
pean G TG raereale ere
W Gini Afgseceale ioeae
Am G Go |....e.[...ee-
WwW 8. voll amewes | Seeee
odtavadtin dhs Sd) [Ronee aaeee
BMW SGo | * | *
BSMW At S- Recameltaaece *
At S > eeetesaece
M W GRBGojox| x *
M SM Peon rics:
A s iWalbaiwet
M SR: [eeseeelegenecdh 16
G Mexico? | A RGoj * | x
V. Preropopa.
a
+Cleodora infundi-| Clio caudata, Z......
bulum.
.|Pelagic
B At
| 8 | Lt | Me | |
Number of species in the Coralline Crag according to the original lists of Mr. Searles Wood... ar
Species regarded by Mr. Jeffreys as varieties
EXPLANATION OF PLATE VI.
Plan of the Coralline-Crag Hill at Sutton, Suffolk.
Section through this hill from the river Deben to Shottisham Hall, with branch
section through the principal pits.
Peewee serene ee ser eecseasseHOobosrertessssssrdsresa ses BOstssase
Speciesiadded IbyaiMinwdielineysiesneeccs: ns eaeeesrcesntsrereendeace eran andes caghtoeweeRnematien a easeeeR oF j
Resulting total number Of speCleS sss .svecesvcedcen salen soe scs ons eseispieinsenane acess seiianeegemnese ene Oe REeREa 316
Species for the first time identified as recent, and marked f .......,s0sessseeees jaeerevialt tats wien al svenhine Ob
Quart. Journ. Geol. Soc. Vol. XXVII. Pl. VI.
M HALL.
Rati oeceseaee) ae Some eee ate
F Dangerfield Ith Bedford S Covent Garden
1
1
:
j
4
~~ - _ ~~. a ee ee , = om —
a
Quart. Journ. Geol. Soc. Vol XXVIl. PL.VI
PLAN OF GCORALLINE GRAG HILL.
AT SUTTON, SUFFOLK.
-_ SECTION FROM RIVER DEBEN AT SUTTON TO SHOTTISHAM HALL,
VRam touse FEBRUARY 1868. .
Level of Fld Giffand Shore.
t : Homzontal Scale. Vertical Scale
1 CGS. Rea Crag. Links mo 0 ¢ 1” ile 2 9g Tuas Fork woe arena apn Fat ‘
Horizontal Scale. F Old Quarry. : * Feta IW 360 SN eo SOE Oo 1600 woe Fet
‘ G Red Pit with. 2038 coraiine Gag
i or a er Gmelin Og Daldore Sad
mages UK Red dug Pits. 3D) tendon Clay.
Planned and levelled by M” Miler, by the , ¥ Dangerfiold ith Bedford € vm udm ;
direction of M” PBrauft, CE Ipswich. : ' . : ' :
DAW:ON—SIGILLARIA, CALAMITES, AND CALAMODENDRON.- 147
2. On the Structure and Arrinitres of Stem arta, CaLaMitTEs and
CatamopEnpron. By J. W. Dawsoy, LL.D., F.R.S., F.GS.,
Principal of M°Gill University.
(Read May 11, 1870*.)
[Plates VIT.-X.]
1. SrerenaRta.
The difficulty of arriving at a correct knowledge of the structure
of these curious trees is caused principally by the unequal durability
of the different parts of the stem. It arises from this that some
portions have usually perished, while others were in process of ©
mineralization, and the portions which remain have in a great
degree lost their original form and arrangement. The outer bark,
while extremely durable, was too impenetrable.to be preserved in
any other way than as compact coal. The fibres of the bark and
of the woody axis are often mineralized or imperfectly preserved as
mineral charcoal. The cellular portions of the bark and of the axis
have usually entirely disappeared. Still, imperfectly preserved stems
can be obtained in great abundance in any coal-field by those who
are content to work on such unpromising material.
Probably the finest specimen of a Sigillaria hitherto described is
that of S. elegans, so admirably figured by Brongniart, and which
has long served to give to the student of paleobotany his ideas of
the structure of the genus. Unfortunately, however, Brongniart’s
specimen represents a small or young stem belonging to the some-
what aberrant subgenus Favularia; so that it fails to give an adequate
idea of the structure of the typical fossil Sigillariw, which are
much more common and important, at least in the coal-fields of
Nova Scotia. The structure of these last, as observed in specimens
obtained at the South Joggins, was, I believe, first described by me
in my paper on the Vegetable Structures in Coal, published in the
‘Journal’ of this Society in 1859. The specimens subsequently
figured in the ‘ Journal’ of this Society, and in the ‘ Transactions’
of the Royal Society, by Mr. Binney, under the name of S. vascularis,
belong, in part at least, to types of structure quite distinct from that
of the true Sigillariey.
My own results as to the typical Sigillariw are thus shortly.
summed up in my paper on the ‘Conditions of Deposition of
Coal” + :—“In the restricted genus Szgillaria the ribs are strongly
developed, except at the base of the stem; they are usually much
wanen the discussion on this paper see Quart. Journ. Geol. Soc. vol. xxvi.
p. 490.
t It would seem that the specimens figured by Mr. Binney as Sigillaria
vascularis (Philos. Trans. vol. cly.) belong in part to the axis of a remarkable
Sigillarioid tree, of which specimens have been kindly shown to me by Prof,
Williamson, and in part (especially pl. xxxy. figs. 5 & 6) to the whole stem
of a Lepidodendron. ‘The latter plant has been described by Mr. Carruthers as
Lepidodendron selaginoides.
¢ Quart. Journ. Geol. Soe. vol. xxii. p, 129.
L2
Wek) PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
broader than the oval or elliptical tripunctate areoles, and are striated
longitudinally. The woody axis has both discigerous and scalariform
tissues, arranged in wedges, with medullary rays as in exogens;
the pith is transversely partitioned in the manner 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 the coal, named ‘ bast-tissue.’ The outer bark was usually thick,
of dense and almost indestructible cellular tissue. The trunk, when
old, lost its regular ribs and scars, owing to expansion, and became
furrowed like that of an old exogenous tree.”
It will be understood that this statement refers to the main stems
of the ribbed Sigillarie of the type of S. renzformus and S. Brownz,
so abundant in the coal-formation of Nova Scotia, and that it is made
with especial reference to the conditions of the accumulation of coal
in that province. The evidence on which it is based may be stated
under the following heads :—
Erect Trunks.—The numerous erect stumps of Sigillarie occur-
ring at the South Joggins, and at Sydney, Cape Breton, are usually
preserved as casts in sandstone, the only part of their organic sub-
stance remaining being the outer bark, which exists in the state of
compact coal. Still the interior structures have not altogether pe-
rished, but may be recognized as a layer of mineral charcoal in the
bottom of the stony column, under the sand and cther foreign mat-
ters subsequently introduced. Occasionally the bark of the tree has
collapsed before it could be filled with sediment, and the only re-
mains of the trunk consist of the little mound of carbonaceous mat-—
ter derived from the tree itself. Cases of this kind are mentioned
in my paper on the South Joggins*. In addition to the coaly mat-
ter showing stracture, we can also occasionally find in the interior of
such erect trees a transversely striated sandstone cast (Sternbergia)
representing the medullary cylinder. In one instance only have I
found the medullary cylinder calcified in such a manner as to show
its structure, and surrounded by the woody cylinder also in a ecalci-
fied state. This specimen was that described, but not adequately
figured, in my paper on the Structures in Coal, and I now propose
to figure it more in detail (Plate X.). . Ordinarily the coaly mass
consists of confused fragments of mineral charcoal derived from
the wood and the fibrous tissues of the bark; but these often retain
their structure very perfectly.
After collecting and examining the woody matter thus remaining
in twenty or more of these erect trees, I have found that, with one
exception, it consists of tissues of a uniform character, presenting
only such differences as might be expected in trees generically
allied. The tissues observed are discigerous or porous wood-cells with
from one to four rows of pores, pseudo-scalariform tissue, and elon-
gated structureless cells of the bark (the “bast-tissue” of my former
papers). These structures indicate that the woody parts of these
trees were identical in character with those of the calcified axis
above-mentioned.
* Quart, Journ. Geol. Soc. vol. x. p. 1.
DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON. 149
' The exception above referred to is, that in one tree, which from
its markings I supposed to be a Sigillaria, the woody tissue was com-
posed of large cells, with many rows of pores (“‘ multiporous tissue ”
of my former papers) of the type of that to which Prof. Williamson
has given the name of Dictyoaylon*. Since, however, as Prof. Wil-
liamson has well shown, such tissue may be regarded as a modifica-
tion of the discigerous variety, and since Corda long ago found it in
the axis of a species of St¢gmariay, there is nothing improbable in the
supposition that we have here merely an indication of a specific or
subgeneric difference coming within the limits of the genus Sigillaria,
as at present understood.
It is to be observed that most of the erect trunks in the coal-for-
mation have not preserved their external markings with sufficient
distinctness to allow the species to be determined by the leaf-scars ;
but they show in most cases the characteristic ribs and rows of
punctures or areoles, modified in the manner which is usual in the
case of old trunks of these plants near their basest.
In Plate VIII. figs. 12,14, 15, 16, I have represented some of the
more usual forms of tissue in the erect Srgillarie.
In Plate X. I have represented the best-preserved axis in my
possession. Fig. 23 shows the structures in the entire stem, except
the portions of cellular bark lost by decay. In the centre is a Stern-
bergia-pith (a). This is surrounded by a woody cylinder (6), the
inner part of which (fig. 24, b 1) consists of scalariform tissue pass-
ing towards the outer surface into pseudo-scalariform (6 2), reticu-
lated with pores (63), and discigerous (64). ‘his woody axis has
medullary rays (figs. 25, 26, 27), and is traversed by bundles of
scalariform tissue proceeding from the inner part of the cylinder.
The outer portion of the inner bark, not seen in this specimen, but in
similar prostrate stems, is composed of elongated thin-walled bast-
cells, with somewhat obtuse ends, and of larger diameter than the
woody fibres of the axis (fig. 29). The tissues of the woody axis
are all arranged in radial series (fig. 28).
Prostrate Trunks.—In the coarse shaly coals, and in the roof-
shales of the ordinary seams, there are often flattened stems of
Sigillaria, having the tissues partially infiltrated with carbonate of
lime or carbonate and sulphate of iron. The tissues usually pre-
served in these flattened trunks are those of the bark, and more
especially its large bundles of elongated or prosenchymatous cells
(‘‘ bast-tissue”’). Of this I have been enabled to obtain very perfect
specimens from these flattened trunks. In a few instances only the
woody structure of the axis remains, showing the same descriptions
of wood-cells already referred to as characteristic of the erect trees.
Plate VIII. fig. 11 is an example of the structures in one of these
prostrate stems.
* Trans. Royal Micro. Soc., Aug. 1869.
t Beitrage zur Flora &c. 1845, pl. xiii. Corda regards this as the structure
of S. ficoides, and the more ordinary variety as that of S. anabathra.
t The species which I have described as S. Browni?, Acad. Geol. 2nd edition,
may be regarded as a representative of these trees.
150 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Sternbergice.—tThe fine specimen of the axis of an erect Stgillaria
already referred to shows that the pith of these trees was of that
transversely laminated character which gives rise to the fossils
known as Sternbergie. Hence we may suppose that some at least
of the numerous casts of Sternbergie found in the Coal-formation
have been derived from Sigillarie ; but this can be ascertained only
by a careful microscopic examination of the remains of woody mat-
ter clinging to the casts. The results of the study of a considerable
number of specimens may be stated as follows :—
(a) As Prof. Williamson and the writer have shown, some of
these Sternbergia-piths belong to coniferous trees of the genus Da-
doxylon. Plate VII. fig. 1 represents a beautifully preserved cylinder
of this kind enclosed in the wood of Dadowylon matertarum.
(5) A few specimens present multiporous tissue, of the type of
Drciyouylon, which, according to Williamson, has a Sternbergia-pith.
Plate VII. fig. 4 affords an instance of this.
(c) Other examples show a true scalariform tissue, comparable with
that of Lepidophloios or Lepidodendron, but of finer texture. Corda has
shown that plants of the type of the former genus (his Lomatophloios)
had Sternbergia-piths. Some plants of this group are by external cha-
racters loosely reckoned bybotanists as ribless Sigqillarie(Clathraria) ;
but I believe that they are not related even ordinally to that genus.
Plate VII. fig. 5 represents a Sternbergia, with tissue partly reticu-
lated and partly scalariform. Plate VIII. fig. 7 represents a speci-
men with true scalariform tissue. Plate VII. fig. 6 is a scalariform
vessel of Lepidophloios drawn to the same scale for comparison. It
will be seen that it is of much coarser texture.
(d). The majority of carboniferous Sternbergie show structures
identical with those described above as occurring in erect Sigillarie.
Such Sternbergie and their structures are represented in Plate VIL.
figs. 2 and 3, and Plate VIII. figs. 8, 9,18. Fig. 8 is a reduced
section of a large flattened tree, apparently a Sigillaria with Stern-
bergia-pith (fig. 9), of great beauty, and not dissimilar from those
sometimes found in the erect Srgillariw. The tissue enclosing it was
unfortunately imperfectly preserved, but had three rows of pores
(fig. 9 a).
Structures in Coal.—The constant association of Sigillaria with
‘the beds of coal, in the underclays, in the roof-shales, and in the coal
itself, is too well known to require any detailed reference; and the
inevitable conclusion that the Stgllaric were the principal plants
concerned in the accumulation of the mineral fuel of the true coal-
measures is generally accepted by geologists. It would naturally
follow from this that tissues of Szgillaria should be more abundant
in the coal than those of other plants. Accordingly, as I have
shown in my paper on the “Structures in Coal,” and on the
“Conditions of Coal-deposition,” tissues similar to those above
described are those which actually occur most abundantly in the
mineral charcoal of the coal-seams. That of the liber or fibrous bark
is perhaps the most abundant of all, and that of the woody. axis the
next in frequency of occurrence.
DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON, 151
It has been held to be an objection to the identification of the
discigerous tissues above mentioned with those of Sigillaria, that
the Stigmarie, when their structure happens to be preserved, show
‘merely scalariform tissue. To this it may be answered :—(1.) That,
as Corda has shown*, some Stigmariew have reticulated or multi-
porous tissues. (2.) The tissue of Stigmaria is not essentially dif-
ferent from the pseudo-scalariform fibres of the stem, and is arranged
in a similar manner, showing that it is homologous rather with
woody than with vascular tissue. (3.) Many Stegmarie probably
belong to Favularia and similar forms, or possibly even to Lepido-
dendroid plantsy. In either case the structure would be unlike that
of the stems of Sigillaria proper. (4.) Inasmuch as the propor-
tions of pseudo-vascular and discigerous tissue may differ greatly
in the stems of Stgzllarie, it would not be unreasonable to suppose
that the tissue, which is more particularly important for the
strengthening of the stem, should be absent, or in a feeble state of
development, in the root. Something of this kind occurs in the
roots of Cycads, and perhaps, if detailed examinations were made,
might be found to be more general than is commonly supposed.
(5.) The outer part of the axis, being left exposed by the decay of
the loose cellular matter of the inner bark, may, in most cases, have
perished. In my specimen of the axis of Sigillaria, above described,
it is in parts much disorganized, and has disappeared, or been con-
verted into coal, on one side.
The evidence included under the above heads is sufficient to show
that the ordinary ribbed Stgillariw referred to in my previous
papers, possessed in their main trunks the following kinds of tissue,
in proceeding from the circumference to the centre :—
(a) A dense cellular outer bark, usually in the state of compact
coal—but when its structure is preserved, showing a tissue of
thickened parenchymatous cells.
(6) A very thick inner bark, which has usually in great part
perished, or been converted into coal, but which, in old trunks,
contained a large quantity of prosenchymatous tissue, very tough
and of great durability. This “bast-tissue” is comparable with
that of the inner bark of modern Conifers, and constitutes much of
the mineral charcoai of the coal-seams.
(c) An outer ligneous cylinder, composed of wood-cells, either
with a single row of large bordered porest, in the manner of Pines
7
* Beitrage zur Flora der Vorwelt.
t Brown, in 1847, described, in the ‘ Proceedings’ of this Society, Stigmaria-
roots of Lepidodendron. Baily seems to have shown that such roots belong to
the singular Lepidodendroid Cyclostigma of the Devonian of Ireland; and
Schimper asserts a connexion of Stigmaria roots with trees which he refers to
Knorria.
{ These are the same with the wood-cells elsewhere called discigerous tissue,
and to which I have applied the terms uniporous and multiporous. The mark-
ings on the walls are caused by an unlined portion of the cell-wall placed in a
disk or depression, and this often surrounded by an hexagonal rim of thickened
wall; but in all cases these structures are less pronounced than in Dadoxylon,
and less regular in the walls of the same cell, as well as in different layers of
the tissues of the axis,
152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
and Cycads, or with two, three, or four rows of such pores some-
times inscribed in hexagonal areoles in the manner of Dadoaylon.
This woody cylinder is traversed by medullary rays, which are
short, and composed of few rows of cells superimposed. It is also
traversed by oblique radiating bundles of pseudo-scalariform tissue
proceeding to the leaves. In some Strgillariw this outer cylinder
was itself in part composed of pseudo-scaiariform tissue, as in Brong-
niart’s specimen of S. elegans ; and in others its place may have been
taken by multiporous tissue, as in a case above referred to; but I
have no reason to believe that either of these variations occurred in
the typical ribbed species now in question. The woody fibres of
the outer cylinder may be distinguished most readily from those of
Conifers, as already mentioned, by the thinness of their walls, and
the more irregular distribution of the pores. Additional characters
are furnished by the medullary rays and the radiating bundles of
scalariform tissue when these can be observed.
(d) An inner cylinder of pseudo-scalariform tissue. I have
adopted the term pseudo-scalariform for this tissue, from the con-
viction that it is not homologous with the scalariform ducts of Ferns
and other Acrogens, but that is merely a modification of the disci-
gerous wood-cells, with pores elongated transversely, and sometimes
separated by thickened bars, corresponding to the hexagonal areo-
lation of the ordinary wood-cells. A similar tissue exists in
Cycads, and is a substitute for the spiral vessels existing in ordinary
Exogens.
(e) A large medulla, or pith, consisting of a hollow cylinder of
cellular tissue, from which proceed numerous thin diaphragms to-
ward the centre of the stem.
The structures above referred to may undoubtedly exist in dif-
ferent proportions in different specics, and also in the same species
in different parts, and at different stages of growth. In the woody
axis more particularly, there 1s evidence that in such forms as S.
(Lavularia) elegans, the scalariform, or pseudo-scalariform, tissues
were predominant. In young stems also, and in roots, this would
probably be the case; and in the latter the texture was much
coarser than in the stem; and, further, Prof. Williamson has
shown me specimens from the Lancashire coal-field, which I have
no doubt are Sigillarioid trees of the type of S. vascularis of Bin-
ney, and which, instead of a Sternbergia pith, have scalariform cells
and vessels in the centre, and in which the bundles of scalariform
vessels traversing the wood are included in considerable masses of
cellular tissue, elongated vertically, like medullary rays. This
plant presents external markings of the Clathraria-type. Mr.
Carruthers has also shown me a specimen ribbed externally, and
apparently a Sigillarca or Syringodendron, which shows only a
cylinder of large scalariform fibres similar to those of Stigmaria.
These facts show how wide differences may exist in the structures
of stems referred by their superficial markings to Stgillaria.
In the case of specimens showing structure merely, it will un-
doubtedly require much further investigation to enable us always to
DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON. 153
distinguish the structures characteristic of the subgenera of Siqil-
laria, or absolutely to separate these from those of certain peculiar
conifers on the one hand, and from those of the higher acrogens on
the other. Young and succulent stems of Dadoawylon may have
much resembled Sigilluria in their structure. Young stems of
Sigillaria proper may have approached closely to those of Favu-
laria ; and since I have shown* that the branches of Favularia
resemble Clathraria in their scars, this last may have presented a
still feebler type of internal organization. Further, there is, as I
have already stated, reason to believe that some of the species
referred by paleobotanists to the Clathraria-division are really
forms of Lepidophloios. These difficulties, in connexion with the
defective state of preservation of specimens, may excuse many differ-
ences of opinion, though I think the facts already stated in this paper
are sufficient to put all students of the subject on the right track in
regard to at least one leading type of these plants, and to remove
some of the more fruitful sources of error.
We may now proceed to inquire what light the structures of
Sigillaria throw on its affinities. On this question, taken in its
-most general aspect, there have, I believe, in modern times been
only two opinions, the views as to alliance with Huphorbia and
Cacti held by some older botanists having been given up. Some
botanists, conspicuous among whom is Brongniart, hold that Szgil-
larie were gymnospermous plants, allied to Cycadacez. Others are
disposed to regard them as acrogens, and as closely related to Lyco-
podiaceee.
In favour of the latter view may be urged the apparent associa-
tion with Sigillaria of certain strobiles resembling those of Lepido-
phloios, the points of resemblance between the tissues of Favularia
elegans and those of Lepidodendron, and the resemblance of certain
Sigularie, or supposed Sigillarie, of the Cluthraria-type to Lepido-
phloios. .
In favour of the former view, we may adduce the exogenous
structure of the stem of Sigillaria, and the obvious affinity of its
tissucs to those of Conifers and Cycads, as well as the constant
association with trees of this genus of the evidently phanerogamous
fruits known as Trigonocarpum and Cardiocarpum. On the other
hand, the resemblance to Lepidodendron may be shown to depend
merely on comparisons of a part of the tissues of Sigillaria with
those of that genus. Grave doubts may also be entertained as to
whether strobiles of Lepidophloios, and even stems of that genus have
not been improperly mixed up with Sigillaria.
It is probable that all botanists who have studied these plants,
might agree that, if not Gymnosperms, they at least present points
of affinity with them, and might be regarded as in some sense a
link connecting them with Acrogens. Supposing this much to be
admitted, important questions remain as to their possible relations to
the modern Conifers and Cycads. The higher S7gillariw unquestion-
A Conditions of Deposition of Coal,” Quart, Journ. Geol. Soc. vol. xxii.
p- 180
154 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
ably resemble Cycads in the structure of their stems. Their long
rigid narrow leaves may be compared to single pinne of the leaves
of Cycads. Their cord-like rootlets, as I have ascertained by actual
comparison, are similar to those of Cycads. If their fruit was of the
nature of Cardiocarpum or Trigonocarpum, this also would corre-
spond. They differed principally in the division of the stem below
into those remarkable underground branches, the Stigmarie, and in
the great upward extension and, in some instances at least, ramifi-
cation of the stem. The former may be regarded as a special modi-
fication connected with their peculiar habitat. The latter may be
interpreted as a modification either tending backward to the Lycopo-
diaceze or forward to the Conifer. Since, so far as we at present
know, the ramification prevails chiefly in the lower forms, the
former may be the more correct view. It is even possible that the
Sigillarve may include forms bridging over the space between the
higher Acrogens and the Gymnosperms. Viewed in this way, the
typical ribbed Sigillarie point downwards through Calamodendron
and Calamites to the Equisetacee, and the Favularia- and Clathraria-
types point through Lepidophloiosand Lepidodendron to Lycopodiacez.
In the upward direction their affinities point both towards Conifers
and Cycads. As our knowledge of the structure of individual species
of Sigillanva increases, we may hope more certainly to trace the links
of these affinities. It is, however, to be observed here, by: way of
caution, (1) that, of the plants reckoned among the several genera or
subgenera of Sigillarie, some may eventually prove to be gymno-
spermous and some cryptogamous, and (2) that, as we shall find in
the next group to have been actually the case, some of these plants
may, with a cryptogamous fructification, have presented a structure
of stem more complex than that found in modern plants of similar
grade.
2. CALAMODENDRON and CALAMITES.
Calamites are among the most abundant fossils of the Carboni-
ferous period, and occur also in the Devonian; and from their pecu-
liar habitat and mode of growth, they are not only preserved as
flattened stems, but also occur in immense numbers standing on the
beds on which they grew.
They have naturally been regarded from the first as allied to
Equisetacee ; and this opinion is ably and, indeed, conclusively
maintained by Schimper in his recent work*, and has been illus-
trated by the recent description of the fruit by Mr. Carruthers.
Difficulties have, however, arisen from the fact that some stems
regarded as Calamites have been found to be surrounded by a thick
woody cylinder composed of discigerous and pseudo-scalariform
tissue, similar to that of the type of Sigillaria above described.
Some botanists have regarded these last as distinct from the true
Calamites, and have placed them in the genus Calamitea, Cotta, or
Calamodendron, Brongniart ; and Williamson has recently proposed
* Paléontologie Végétale.
DAWSON—-SIGILLARIA, CALAMITES, AND CALAMODENDRON. 155
the name Calamopitus* for a group believed to be intermediate be-
tween Calamodendron and true Calamites. On still other grounds,
Bornia and other genera or subgenera have been separated from Cala-
mutes proper. Latterly Schimper has endeavoured to combine the view
of the Equisetaceous affinities and annual growth of the stems of
Calamites with what, at first sight, seems the totally irreconcilable
woody character of the stem of Calamodendron as described by
Cotta, Dawes, and Binney.
In all my own publications on this subject, from the date of ae
first paper on Calamites published in the Journal of this Societyy, I
have held that Calamites proper are Equisetaceous plants, having
the external characters of their stems preserved, and that in the last
respect they differ from the internal casts which belong to Calamo-
dendron. All my subsequent observations have served to confirm
these conclusions, which I would now illustrate by the following
considerations.
1. The true Calamites (e.g. C. Suckoun, C. canneeformis, C. Cistit,
&e.), when well preserved, present, externally, somewhat flat smooth
striated ribs, with distinct nodes, and having, at the upper end of
each rib, a rounded areole with a central dot or scar, marking the
disarticulation of a leaf, branchlet, or root, or, in some cases, the ex-
tremity of one of those radial prolongations of the pith which have
been described by Williamson. In one specimen in my possession
there is a double set of marks—smaller ones on the node, apparently
belonging to the appendages, and larger marks below the node, which
may represent the radial prolongations of the pith (Pl. X. fig. 22). The
cortical investment is very thin and dense, and presents externally
the characters of an epidermis, not showing, as in the case of Stern-
bergia or Calamodendron, a coating of woody fibres externally, and
therefore cannot be regarded as a mere medullary sheath or, as
Schimper supposes, the ‘membrane lining the hollow interior of the
stem. I may remark here, that erect Calamites are sometimes sur-
rounded by a calcareous or ferruginous concretionary coating which
must not be confounded with the true surface of the stem.
2. The ordinary Calamites are seen to stand erect, rooted zn situ,
and attached together at the bases, or arising from rhizomata. The
stems can be seen to bud from each other; and the roots can be
traced proceeding from their bases and lower nodes. Figures of erect
specimens were given in my paper on Erect Calamites, and also in
that on the South Jogginst. Abundant specimens may be obtained
in the magnificent petrified Calamite brakes at the last-mentioned
locality, and, I venture to say, cannot be studied by any geologist
without producing the conviction that the erect cylindrical casts im-
bedded in groups in the sandstone must represent the true external
form of the plant. I have also shown, in the paper above cited, that
these erect stems are crushed by lateral pressure, and broken down
* Preoccupied by Unger for certain Devonian plants.
t On the Occurrence of Upright Calamites near Pictou, Nova Scotia, Quart.
Journ. Geol. Soc. vol. vii. p. 194.
$ Quart. Journ. Geol. Soc, vol. vii, p. 194, and vol. x. p. 1.
156 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
and flattened at the top, exactly as somewhat strong fistulous stems
would be. It is obviously impossible that casts of medullary cavities
could be preserved in this manner. Neither Sternbergie nor casts of
the pith of Calamodendra ever occur under such circumstances.
3. The stems of Calamites may be seen to have produced leaves
and branchlets in such a manner as to prove that they are complete
stems preserving their external surface. In my paper on the South
Joggins, I figured and described the leaves of C. Cistw as seen
attached to the erect stems. I have since, in ‘ Acadian Geology,’
figured those of C. Suckovzi, found under similar circumstances; and
I have specimens which appear to me to verify the figure given by
Lindley and Hutton of the leaves of C. nodosus. I have also ob-
tained beautifully preserved specimens of the leaves of C. transi-
tionis, a species common to the Devonian and Lower Carboniferous.
It has been supposed that the scars on the nodes of Calamites are
merely the marks of bundles of vessels passing from the interior to-
wards the surface; but it is obvious that, in the case of stems actually
producing leaves and branchlets, this cannot be the true explana-
tion, though after seeing the very instructive slices of Prof. William-
son’s Calamopitus, kindly shown to me by him, I am prepared to
admit that in some specimens, at least, they may represent the
“medullary radii,” which, as already stated, sometimes appear m
addition to the true vascular scars.
4, The leaves of Calamites were not, as is often stated, identical
with those of Asterophyllites; and the genus Calamocladus, in which
Schimper has placed many plants of the latter genus, is therefore
altogether unnecessary. A careful microscopic examination of the
leaves which I have found attached to Calamites convinces me
that they have distinct characters, and affords an additional link
of connexion with Equisetacese. The leaves of Asterophyllites proper
are flat, expanded in the middle, and with a distict midrib. Those
of Calumites are strictly linear, thick, and angled, and are be-
sides marked with transverse lines or strie. Similar transverse
lines occur on the branchlets of some modern Hquiseta, and are
produced by lines of minute stomata. Well-preserved specimens of
Calamite-leaves have precisely the same appearance, so that they
may be compared to branchlets of Hquescta deprived of their sheath.
Flattened leaves of Calamites, it is true, sometimes present the ap-
pearance of a midrib; but this arises either from the prominence of
the upper angle, or the appearance of an internal axis through the
substance of the leaf. Unless very badly preserved, they can always
be distinguished from Asterophyllites or Annularia. The connexion
supposed, by Ettingshausen and others, to obtain between Calamites
and Asterophyllites has arisen either from accidental association,
or from failure to distinguish leaves and stems of Calamites from the
corresponding parts of Asterophyllites*, The conjecture of Brong-
niart that some, at least, of the Asterophyllites may be leaves, not of
* The species Asterophyllites comosus, L. v. H., appears to consist of, or to in-
clude, leaves of Caiamites; and there is reason to doubt whether the proper,
Asterophyllites should be separated from Annularia,
DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON. 157
Calamites, but of Calamodendron, rests on different grounds, and is
supported by the fact that some of the larger stems which may be
supposed to represent the external surface of Calamodendron, have
tumid nodes similar to those of the branches of Asterophullites.
Stems of this kind are sometimes found in an erect position in the
Coal-measures of Nova Scotia, and are manifestly distinct from those
of ordinary Calamites.
~ 5. The microscopic structure of Calamites is not precisely iden-
tical with that of Calamodendron, though the latter may be regarded
as a more advanced type of the former. The Calamites have a thin
outer coat with lacune, or air-cells, like those of modern Hquiseta ;
and the tissue intervening between these contains large vasiform
tubes marked on the surface with numerous rows of small pores
(“multiporous tissue” of my papers on the Structures in Coal,
&e.), and which bear some resemblance to the fibres of Dicty-
oxylon as described by Williamson (PI. IX. fig. 19). This strue-
ture has been illustrated by Goeppert, Unger, Schimper, and others ;
and I have verified it by the microscopic examination of numerous
flattened Calamite-stems in the shales and coarse coals. Facts of
this kind kind were mentioned in my paper on the ‘Structures in
Coal.’
The Calamodendra, on the other hand, are casts of the medullary
cavities of stems having a thick woody envelope disposed in wedges
separated by intervening tracts of cellular tissue, which, according
to Williamson, are of the nature of large medullary rays, while
smaller medullary rays occur in the intervening wedges, and pre-
senting the same discigerous and pseudo-scalariform tissues ob-
served in Sigillarta. Ihave represented in Plate IX. two forms of
Calamodendron with the tissues found attached to them. These
stems, no doubt, have lacunz like those of Calamites, and resemble
them in general arrangement of parts, but differ in the much greater
development of the woody tissue, and, in some species at least, in
the character of this tissue.
6. The fructification of Calamites I have not found in connexion
with the stems. I have no doubt, however, that some of the spikes
of fructification described by authors as the fruit of Calamites, really
belong to these plants. There has, however, been some confusion
between the fruit of Calamites and Asterophyllites, which demands
attention from those who have access to the specimens.
It results from the facts above stated that the true equisetaceous
Calamites are well known to us by their external forms, habit of
growth, and foliage, as well as by their internal structure ; and on
all these grounds no reasonable doubt can be entertained as to their
affinities. Whether, as Schimper supposes, they were merely an-
nual stems like those of modern Equiseta, admits of more doubt. In
the equable climate of the Coal-period such stems may have con-
tinued growing from year to year. Nor do I think that their rhi-
zomata were relatively so important as those of Hquiseta. In some
of the species, at least, the erect stem itself, fortified by adventitious
roots, and partly buried by increasing deposits of sediment, seems to
158 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
have served the purpose of a rhizoma*, The best example that. I
have seen of the rhizoma of a Calamite is that figured in Plate IX,
(fig. 21), from a specimen presented by me to the Geological Society
many years ago.
With regard to Calamodendron the difficulties are greater, and
have been well stated by Prof. Williamson in a recent paper in the
‘ Memoirs of the Literary and Philosphical Society of Manchester’ +,
in which he describes under the generic name Calamopitus a peculiar
stem, which, while he identifies it in its general characters with
Calamites, he justly regards as being in internal structure distinet
from the Calamodendra described by Cotta and Binney.
The characters of Calamodendron as distinguished from ordinary
Calamites may be summed up as follows :—
(a) The part usually preserved is the internal axis, corresponding
to a Sternbergia. It presents ribs similar to those of Oalamites, but
more angular, and almost always haying traces of woody fibres capa-
ble of showing the structure on some part of their surface. I have
not seen on these casts any distinct traces of scars or areoles. These
casts of the pith of Calamodendron constitute the greater part, if not
the whole of the specimens referred to C. approaimatus.
(6) More complete specimens are invested with woody matter,
arranged in wedges, and consisting of elongated cells and porous,
discigerous, or pseudo-scalariform tissue. My specimens do not
show distinctly the arrangement of these; but this has been well
described by other observers. Williamson describes medullary rays
in the woody bundles in addition to the large cellular tracts inter-
vening between them.
(c) The actual external surface of Calamodendron is not certainly
known; but I have been disposed to regard as of this kind those
ribbed stems, found in the coal-formation, which have swollen nodes
as if caused by the emission of whorls of small branches. I have
specimens of these in my collection, which I have hesitated to name
or describe until they could be better understood. Prof. Williamson’s
description of Calamopitus now inclines me to suppose that they be-
long to that genus or to allied forms.
With regard to the affinities of the Calamodendra, the structure of
the stem raises them above the Calamites and modern Hquiseta, and
justifies the conjecture of Brongniart that they may have been gymno-
sperms. Williamson, Carruthers, and Binney, however, attribute to
them a cryptogamous fructification. In this case they may, as the
former suggests, be a connecting link between Acrogens and Gymno-
sperms. Should subsequent investigations confirm this view, it will
throw an interesting light on the possible affinities of Sigillarza.
Calamites, on the one hand, and Lepidodendron on the other, are
distinctly cryptogamous and are related to, or included in, the mo-
dern families of Equisetaceze and Lycopodiaceze. But Calamodendron
seems to form a connecting link between Oalamites and the ribbed
’ Sigillarie; and in like manner Lepidophloios seems to connect the
* See my description in Quart. Journ, Geol. Soe, vol. x.
t Vol. iy. drd Series.
DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON. 159
Lepidodendra with the Sigillariw of the Favularia-type. On the
other hand, as already stated under Sigillaria, the ribbed Sigillarie
may be related through Ormowylon and Dadoaylon to the modern
Conifers, and the Favularie may be related to the Cycads. ‘This re-
lationship may be expressed as follows :—
Cycadacee. Oonifere.
Dadoxylon.
Favularia ? Paleoxylon.
Ormoxylon 7.
Dictyoxylon.
SIGILLARIA.
Rhytidolepis. Calamodendron.
Favularia ? Calamopitus.
Clathraria. -Bornia.
Syringodendron. Calamites.
Lepidophloios. Hquasetacee.
Lepidodendron*.
Lycopodiacee.
I do not give this Table with any view to theories of derivation,
but merely as an expression of probable affinities among these very
curious and ancient types of vegetation.
T may add here a few words with reference to Sphenophyllum, a
genus which some authors unite with Calamites. The verticillate,
cuneate, veiny ieayes of this plant, and its spikes of fructification
have long been known; and in 1865 I was enabled by a specimen
in the collection of Sir W. E. Logan to determine the structure of
its stem, which contains a slender axis of reticulato-scalariform
vessels of the type of those in Zmesipterist. These plants obviously
had no connexion with Calamites or Calamodendron, but constitute
a peculiar synthetic type, presenting points of resemblance to Ferns
and Marsiliacecze.
In conclusion, and with reference to my former papers on the
“ Structures in Coal,” I would repeat the statement made in those
papers, that the tissues of Sigzllaria, as defined in this paper, and of
Calamodendron enter more largely than any others into the compo-
sition of the mineral charcoal, and other parts retaining structure,
of the coal of Nova Scotia ; and I have reason to believe that similar
tissues are at least very abundant in the coal of this country.
Supplementary Note-—Owing to the delay in the publication of the
above paper, it is necessary to add the following statements :—
(1) Prof. Williamson has described another type of Calamitean
stem, which he regards as intermediate between his Calamopitus and
Calamodendron §, but which has the reticulated or multiporous vessels
of the former. To Prof. Williamson is due the credit of recognizing
this structure for the first time in English specimens, though, as above
* Tncluding Sagenaria. tT Dawson, MS.
t Quart. Journ. Geol. Society, May 1866.
§ Manchester Lit. and Phil. Soc. Proceedings, 1870.
160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
stated, it had previously been well known elsewhere. I regard these
plants, so well described by Williamson, as true Calamites, in the
sense in which that word is used above.
(2) The same paleobotanist has independently expressed the be-
lief above stated, that the leaves of Calamites are distinct from those
of Asteroph yllites, and has also stated a distinction between those so-
called Volkmannice which may be regarded as fruits of Calamites
and those which belonged to Asteroph yllites *, He hasalso described
a specimen of Stigmaria showing the medullary rays, and otherwise
approaching to the structures which should be found in the roots of
the typical Sigillarie above described.
(3) Schimper, in his ‘ Paléontologie Végétale,’ vol. xi., has treated
the Sigillarie very slightly. He adds no new facts of importance to
their history, does not separate them from the plants of the genus
Lepidophloios, usually mixed with them, refers the whole to one
genus, and places them with the Lycopodiacez.
(4) Binney, in the Paleontographical Society’s Publicalone,
vol. xxiv., has described, under the name of Bowmanites cambrensis,
a very interesting plant, which I regard as a typical member of the
group Asterophyllitee, as distinguished from Calamitec.
(5) Attention having been directed by Prof. Huxley to the pre-
sence of spore-cases in Coal, I have endeavoured to show, in a paper
in the ‘ American Journal of Science’ for April, that these bodies are
not a large constituent of ordinary Coal, and that any importance
which they possess in this respect is due to their identity in chemical
composition with those cortical and epider mal tissues which, like the.
suberin of cork, are more nearly allied in composition to Coal than
any other recent vegetable matters, and better fitted, by their che-
mical and mechanical properties, for its production.
EXPLANATION OF THE PLATES.
Prats VII.
Fig. 1. Sternbergia, pith of Dadoxylon; 1 a, section of one side, showing
diaphragms; 1 0, section of a diaphragm and three wood- cells,
magnified; 1c, two wood- cells, highly magnified, showing reticu-
lated walls.
Sternbergia, pith of Sigillaria, natural size; 2a, 2, discigerous
tissue investing the same.
Sternbergia, pith of Sigillaria, natural size; 3a, discigerous and
scalariform tissue.
Sternbergia, natural size; 4 a, reticulato-scalariform tissue.
. Sternbergia, natural size; 5a, 5, scalariform and reticulato-scalari-
form tissue.
6. Scalariform vessel of Lepidophioios.
op 99 bo
Prats VIII. "
Fig. 7. Sternbergia, of Lepidodendroid tree?, natural size; 7a, scalariform
tissue.
8. Section of a flattened stem (Sigéldaria ?) 1 foot in diameter, converted
into coal, with Sternbergia-pith.
* Manchester Lit. and Phil, Soc. Proceedings, Feb, 1871.
Quart. Journ. Geal. Soc. Vol. XXVIL PL VIL
LLANE pea ae
SoS}
oboe
W.G_Snnth hth. Mantern Bro® amp.
STERNBERGIA.
Quart.Journ. Geal. Soc. Vol. XXVIL PL VUE
‘Mintern Bro® imp
W.G. Smith Ith.
STERNBERGIA.
Ae
4 “
Quart. Journ. Geal. Soc. Vol XXVIL. PL.IX
Mimtern Bro? imp.
W. G. Smmth hth.
CALAMODENDRON & CALAMITES.
Quart. Journ. Geal. Soc. Vol. KXVIT PL X.
135)
Mintern Bro* imp
W.G. Smith hth.
SIGILLARIA.
ou
Fig. 9.
10.
11.
12.
13.
14,
“DAWSON—SIGILLARIA, CALAMITES, AND CALAMODENDRON.. 161
Sternbergia, pith of the same, natural size; 9 a, discigerous tissue of the
same.
Another stem, probably Coniferous, with Sternbergia pith.
Woody tissue of prostrate Sigz/aria ; 11a, bast-tissue of the same.
Woody tissue of a Sigillaria; 12 a, medullary ray.
Tissue of a Sternbergia similar to fig. 9.
15, 16. Discigerous tissue of erect trees (Sigillarig) in mineral charcoal.
Prats IX,
Fig. 17. Calamodendron approximatum, cast of pith; 17a, 170, discigerous and
18.
Fig. 23.
on one
VOL.
scalariform tissue of the same.
Calamodendron invested with woody tissue: A, pith; B, woody cylinder ;
18a, cross section ; 180, cross section, magnified, showing compression
of the tissue; 18c, discigerous and pseudo-scalariform tissue of the
same.
. Portion of a multiporous vessel of a true Calamites, magnified to the
same scale with figs. 17a & 178.
. Stem of erect Calamodendron (S. Joggins, Nova Scotia), showing its
external surface, one-third nat. size.
. Base of stem of Calamites (8, Joggins), showing rhizoma, reduced.
22.
Node of Calamites, showing scars of verticillate branchlets and of radial
processes.
Puate X.
Radial section of stem of Sigillaria of the type of S. Browniz, Dawson,
restored, natural size: @, pith; b, woody cylinder; c, cellular inner
bark; d, fibrous bark ; e, outer cortical layer.
. Radial section of the woody cylinder, magnified (letters as above); and
portions of the tissues more highly magnified below: 01, inner pseudo-
scalariform cylinder ; 62, 3, 4, discigerous outer cylinder.
. Radial section, more highly magnified, showing one of the radiating
bundles of vessels (this section has been inverted) ; 25a, single pseudo-
scalariform vessel from radiating bundle.
. Tangential section of the same stem, showing the woody fibres and one
27.
28.
29.
Note.
of the radial bundles, and the medullary rays.
Tangential section showing woody fibres and medullary rays, more
highly magnified.
Radial arrangement of woody fibres, magnified.
Fibres or elongated cells of the bark (d).
a the drawings of separate fibres and vessels in the above figures are
scale. ;
XXVII.—PART f. N
162
DONATIONS
TO THE
LIBRARY OF THE GEOLOGICAL SOCIETY.
From October 1st to December 31st, 1870.
I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.
Academy (Journal), Vol.ii. Nos.8—14. May to November 1870.
American Journal of Conchology. Vol. v. No. 3.
American Journal of Séience and Arts. Second Series. Vol. 1.
Nos. 148-150.
T. S. Hunt.—On the probable seat of Volcanic Action, 21.
W. T. Reepper.—Notice of some Minerals from New Jersey, 35.
On the Occurrence of a Peat-bed beneath deposits of Drift of South-
western Ohio, 54.
T. S. Hunt.—On the Geology of Eastern New England, 83.
C. U. Shepard, sen.—Mineralogical Contributions, 90.
O. C. Marsh.—Notice of a New Species of Gavial from the Eocene
of New Jersey, 97.
R. Brown.—On the supposed absence of the Northern Drift from the
Pacific Slope of the Rocky Mountains, 318.
American Naturalist. Vol. iv. Nos. 8-10. October to December
1870.
J. W. Foster.—Recent Advances in Geology, 449.
L. Agassiz.—The former Existence of Local Glaciers in the White
Mountains, 550.
Atheneum (Journal). Nos. 2240-2251. October to December
1870.
Belfast Naturalists’ Field-Club. The Seventh Annual Report.
1869-70.
DONATIONS. 163
Berlin. Monatsbericht der kénigl.-preussischen Akademie der Wis-
senschaften zu Berlin.
——. “Zeitschrift der deutschen geologischen Gesellschaft. Band
xxii. Heft 3. 1870.
F. J. Wiirtemberger.—Die Tertiirformation im Klettgau, 471 (1
late).
Pe Tebe Python Euboicus, eine fossile Riesenschlange aus
tertidrem Kalkschiefer von Kumi auf der Insel Eubcea, 582 (1
plate).
G. vom Rath.—Geognostisch-mineralogische Fragmente aus Italien,
3. Theil, 591 (2 plates).
H. Laspeyres.—Das fossile Phyllopoden-Genus Leaia, R. Jones, 733
(1 plate).
A. Kenngott.—Ueber den Palatinit von Norrheim in der Pfalz, 747.
G. Rose.—Ueber ein Vorkommen von Zirkon in dem Hypersthenit
des Radauthals bei Harzburg, 754.
Zeitschrift fiir die gesammten Naturwissenschaften. Neue
Folge. Bandi. 1870.
H. Credner.—Geognostische Aphorismen aus Nordamerika, 20 (1
late).
B Kiisel—Die Tertiarschichten iiber den Septarienthone bei
Buckow, 208.
O. Lenz.—Ueber das Auftreten jurassischer Gebilde in Bohmen, 337
(2 plates).
T. Liebe.—Die Knochenlagerstatte von Pahren im reussischen Ober-
lande, 33.
A. Schreiber.—Keuper, Liasthon und Sandstein in der Umgebung
Ummendorfs, 488 (1 plate).
F, Schonichen.—Galmeigange im Jurakalk auf der cantabrischen
Kiiste in Spanien, 382.
——. Die Kieslagerstitten der Provinz Huelva in Spanien, 391.
M. Siewert.—Ueber Phosphorkupferverbindungen, 38.
Calcutta. Asiatic Society of Bengal. Journal. New Saniey. Vol.
xxxix. No. 162.
——. ——. Proceedings. Nos. 7&8. July and August 1870.
Canadian Journal. NewSeries. Vol. xii. No. 6. October 1870.
E. J. Chapman.—A Table for calculating the Weight and Yield,
per Running Fathom, of Mineral Veins, 478.
Chemical News. Vol. xxii. Nos. 567-576. October to December
1870.
Colliery Guardian. Vol.xx. Nos. 510-520. October to December
1870. :
Copenhagen. Det Kongelige danske Videnskabernes Selskabs Natur-
vidensskabelige og Mathematiske Afhandlinger. Fifth Series.
Vol. viii. Parts 6 & 7. Vol. ix. Part 1. ;
Oversigt over det Kongelige danske Videnskabernes Selskabs
Forhandlinger. 1868, No.6; 1869, No. 4.
mM 2
164 DONATIONS.
Copenhagen. Oversigt over det Kongelige danske Videnskabernes
Selskabs Forhandlinger. 1870, No. 1.
F, Johnstrup.—Jordskjzlvet i Sjelland den 28 Januar 1869, 1
(1 plate).
Cotteswold Naturalists’ Field-Club. Proceedings for 1869.
W. C. Lucy.—The Gravels of the Severn, Avon, and Evenlode, and
their extension over the Cotteswold Hills, 71.
T. Wright.—On the Correlation of the Jurassic Rocks, in the
Department of the Céte-d’Or, France, with the Oolitic formations
in the counties of Gloucester and Wilts, England, 143.
Devonshire Association for the Advancement of Science, Literature,
and Art. Report and Transactions. Vol.iv. Part 1. 1870.
W. Pengelly.—The Ash-Hole and Bench Bone-caves at Brixham,
South Devon, 73.
——. The Literature of the Caves near Yealmpton, South Devon,
81.
Notes on Vessels made of Bovey Lignite and of Kimmeridge
Coal, 105.
P. F. 8S. Amery.—Stones found at Swincombe (Dartmoor), probably
connected with Ancient Mining there, 136.
KE. Parfitt—Fossil Sponge-spicules in the Greensand of Haldon and
Blackdown, 138.
W. Pengelly.—The Modern and Ancient Beaches of Portland, 195.
E. TA mene occurrence of Fossils at Smuggler’s Cove, Torquay,
291.
R. Kirwan.—Notes on the Pre-Historic Archeology of East Devon,
295.
W. Whitaker.—List of Works on the Geology, Mineralogy, and
Paleontology of Devonshire, 330.
Dresden. Sitzungs-Berichte der naturwissenschaftlichen Gesellschaft
Isis in Dresden. 1870. April to June.
Dublin. Journal of the Royal Dublin Society. Vol. v. No. 39.
1870.
Geological Magazine. Vol.vii. Nos. 10-12. October to December
1870.
D. Mackintosh.—Surface-geology of the Lake-district, 445 (2 plates).
T. Davidson.—Italian Tertiary Brachiopoda. Part i1i., 460 (1 plate).
G. Dowker.—On the Chalk of Thanet, Kent, &c., 466.
H. B. Medlicott.—On Faults in Strata, 473.
H. Woodward.—Contribution to British . Fossil Crustacea, 493 (1
late).
w C. ae Post-Pliocene Drift of Charnwood Forest, 497.
W. Mundle.—On the Coal-bearing Rocks of Southern Chile, 499.
H. F. Hall.—The Glacial Deposits of Llandudno, 509.
L. C. Miall.—Swallow-holes in the Mountain Limestone, 513.
E. Wilson.—Altered Clay-bed, Tideswell Dale, Derbyshire, 520.
J. Prestwich.—Notes on Earthquakes, 541.
C. Eyton.—On the Age and Position of the Blue Clay in the West
of England, 545.
DONATIONS. 165
Geological Magazine. Vol. vii. Nos. 10-12 (continued).
G. Maw.—On Recent Changes of Level in the Coast-line of the
Mediterranean, 548.
H. Woodward.—Contributions to British Fossil Crustacea, 554 (1
late).
J. i Walker—On Secondary Species of Brachiopoda, 560 (1 plate).
D. Mackintosh.—Dispersion of Granite-blocks over the Plain of
Cumberland, 564. ;
Geological Survey of Ireland, Sheet 95, by G. H. Kinahan and J.
Nolan, noticed, 485. :
J. Geikie.—On the Carboniferous Formation of Scotland, noticed,
485,
Papers read in Section C, British Association, Liverpool, noticed,
523.
G. H. Morton’s ‘Glaciated Condition of the Triassic Rocks around
Liverpool,’ noticed, 525. :
‘Mountain Limestone of Flintshire and Denbighshire,’ noticed,
526.
T. Wright’s ‘ Comparison of the Céte-d’Or, in France, with the Cot-
teswold Hills,’ noticed, 568.
J. Croll’s ‘Cause of the Motion of Glaciers,’ noticed, 572.
Barrande’s ‘ Cephalopoda of Bohemia &c. Distribution of the Class,’
reviewed, 486.
C. F. Hartt’s ‘Geology of Brazil,’ reviewed, 528.
Annual Report of the Director-General of the Geological Survey of
Great Britain &c., reviewed, 531.
Dr. Yeats’s ‘ Natural History of Commerce,’ reviewed, 533.
W. Carruthers’s ‘ Fossil Cycadean Steins,’ reviewed, 573.
Journal of the Royal Agricultural Society, reviewed, 577.
Reports and Proceedings of Societies, 491, 579.
Correspondence, 535, 583.
Miscellaneous, 540, 587.
Iron and Coal Trades Review.. Vol. iv. Nos. 186-146. October
to December 1870.
Journal of the Chemical Society. Vol. viii. October to December
1870.
Linnean Society of London. Journal. Zoology. Vol. xi. No. 49.
London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xl. Nos. 267-269. From Dr. W. Francis, F.GS.
Longman’s Notes on Books. Vol. iv. No. 63. November 1870.
Monthly Microscopical Journal. Vol.iv. Nos. 22-24. October to
December 1870.
Moscow. Bulletin de la Société Impériale des Naturalistes de Mos-
cou-,, E870. No.7:
Munich. Abhandlungen der koniglich-bayerischen Akademie der
Wissenschaften. Mathematisch-physikalische Classe. Band x.
Abth. 3.
166 DONATIONS.
Munich. Sitzungsberichte der kénigl.-bayer. Akademie der Wissen-
schaften zu Miinchen. 1870. Band u. Hefte 2-4.
Giimbel.—Ueber den Riesvulkan und tber vulkanische Erscheinun- _
gen im Rieskessel, 153.
C. Nollner.—Ueber den Liineburgit in Harburg, 291.
C. v. Kobell.—Ueber den Giimbelit, ein neues Mineral yon Nord-
halben bei Steben in Oberfranken, 294.
Nature (Journal). Vol. ii. Nos. 49-52. October 1870.
Eruption of the Volcano Tongariro, New Zealand, 477.
A. R. Wallace.—The Glaciation of Brazil, 510.
W. B. Carpenter.—The Geological Bearings of recent Deep-Sea
Explorations, 513.
——. Vol.in. Nos. 53-59. November to December, 1870.
The Geology of the Diamond-fields, South Africa, 2.
J. D. Hooker.—Schimper’s Vegetable Paleontology, 42.
The Yosemite Valley and the Sierra Nevada of California, 44.
Neuchatel. Bulletin de la Société des Sciences Naturelles. Tome
villi. Troisiéme cahier. 1870.
A. Chatelain.—Les Houilles en Suisse, 393.
P. Traub.—Les Solfatares de la Mer Rouge, 417.
A. Jaccard.—Quelques Mots sur les Cartes Géologiques et en parti-
culier sur les Feuilles vi., xi., et xvi. de la Carte Géologique de
la Suisse, 432.
Neues Jahrbuch fiir Mineralogie, Geologie, und Paliontologie. 1870.
Hefte 2-5.
D. Burkart.—Die Goldlagerstatten Californiens, 129 (1 ve
J. Hirschwald.—Beobachtungen an Krystallgerippen, ein Beitrag
zur krystallo-genetischen Forschung, 183 (1 plate).
F, Sandberger.—Ueber Glaukopyrit, ein neues Mineral, 196.
G. vom Rath.—“ Der Aetna in den Jahren 1863 bis 1866 mit beson-
derer Beziehung auf die grosse Hruption von 1865 ; ” auszugsweise
iibertragen nach dem Werke von O. Silvestri, 257.
B. Mahr.—Beitrag zur Kenntniss fossiler Insecten der Steinkohlen-
Formation Thiringens, 282.
F. Goldenberg.—Zwei neue Ostracoden und eine Blattina aus der
Steinkohlen-Formation von Saarbriicken, 286.
G. Werner.—Zur Theorie des sechsgliedrigen Krystallsystems, 290.
F. Sandberger.—Ueber zwei neue Phosphate, 306.
©. Klein.—Ueber neue Formen am Bleiglanz, 311.
A. Streng.—Mineralogische Notizen, 314.
K. v. Fritsch.—Vorstudien tiber die jiingeren mesozoischen Ablage-
rungen bei Hisenach, 385.
H. B. Geinitz.—Ueber organische Ueberreste aus der Steinkohlen-
Formation von Langeac, Haute-Loire, 417 (1 plate).
A. Streng.—Mineralogische Notizen, 425.
C. W. C. Fuchs.—Bericht tiber die vulcanischen Hreignisse des
Jahres 1869, 433.
A. Kenngott.—Ueber einen Obsidian vom Hekla auf Island, 529
1 plate).
wnat Uber die Krystall-Gestalten des Dimorphin, 537.
DONATIONS. 167
Neues Jahrbuch fiir Mineralogie, Geologie, und Paliontologie. 1870.
Hefte 2-5 (continued).
F, Scharff.—Ueber den Einfluss des Zwillings-Baues auf die Gestal-
tung der Krystalle des Kalkspathes, 542 (1 plate).
L. Dressel.—Mittheilungen vom Laacher See, 559.
Allgemeines Repertorium der Mineralogie, Geologie, und
Paliontologie fiir das Decennium 1860-69.
Neweastle-on-Tyne. Transactions of the North of England Institute
of Mining Engineers. Vols. i. & ii., vi.-xvill. 1852-69.
Paris. Comptes Rendus hebdomadaires des Séances de |’Académie
des Sciences. Deuxiéme Semestre 1870. Tomelxxi. Nos. 5-8.
F. Pisanii—Analyse de la nadorite, nouvelle espéce minérale de la
province de Constantine (Algérie), 319.
V. Raulin.—Sur le régime pluvial des Alpes frangaises, 326.
Chassin.—Sur un tremblement de terre survenu au Mexique, le
11 Mai 1870, 329.
E. Delesse.—Note sur une carte lithologique de l’embouchure de la
Seine, 349,
Revue des Cours Scientifiyues de la France et de I’Etranger.
Septiéme Année. Nos. 30-41. June to September 1870.
L. Agassiz.—Antiquité Géologique des Continents actuels, 484.
——. Origine des Terrains Erratiques, 484.
Géologie du lit du Gulf Stream. Les Formations Madrépo-
riques du Golfe du Mexique, 485.
Les Bassins sous-Marins et les Bassins Terrestres, 487.
——. Lvolution embryonnaire des Coraux comparée a leur
Classification, 4 leur Succession Géologique et 4 la Profondeur de
leur Habitat actuel, 488.
T. S. Hunt.—Sur le siége probable de l’action Volcanique, 621.
Photographic Journal. Nos. 219 & 220. November and December
1870.
Quarterly Journal of Science. No. 28. October 1870.
H. Woodward.—The Geological Survey of India, 458.
Royal Astronomical Society. Monthly Notices. Vols. xxviii—xxx.
1868-70.
A General Index to the First Twenty-nine Volumes of the
Monthly Notices.
——. Memoirs. Vol. xxxvii. Parts 1 & 2; and vol. xxxviii.
Royal College of Surgeons. Calendar. July 1870.
Royal Geographical Society. Proceedings. Vol. xiv. Nos. 3-5.
Royal Institution of Great Britain. Proceedings. -Vol.v. No. 7.
Vol. vi. Nos. 1 & 2.
C. Moseley.—On the Descent of Glaciers, 155.
168 DONATIONS.
Royal Society. Catalogue of Scientific Papers. Vol. iv. LHE to
POZ. Ato. 1870.
St. Petersburg. Bulletin de Académie Impériale des Sciences de
St. Pétersbourg. Tome xv. Nos. 1 & 2.
Mémoires de l’Académie Impériale des Sciences de St. Peter
bourg. 7™° Série. Tome xv. Nos. 5-8.
N. v. Kokscharow.—Ueber den Olivin aus dem Pallas-Hisen, No. 6
(4 plates).
Society of Arts. Journal. 116th Session. Vol. xvi. Nos. 933-
938; and 117th Session. Vol. xix. Nos. 939-943.
Student and Intellectual Observer. New Series. Vol. i. No. 4.
Stuttgart. Wiirttembergische naturwissenschaftliche Jahreshefte.
1870. Hefte 1-3.
O. Fraas.—Ueber die Entwicklung der vaterlandischen Geologie, 83.
C. Deffner.—Der Buchberg bei Bopfingen, 95 (3 plates).
O. Fraas.—Die Fauna von Steinheim. Mit Rucksicht auf die mio-
cenen Saugethier- und Vogelreste des Steinheimer Beckens, 145
(9 plates).
Vienna. Anzeiger der k.-k. Akademie der Wissenschaften in Wien.
1870. Nos. 21-27.
Jahrbuch der k.-k. geologischen Reichsanstalt. 1870.
Band xx. No. 1.
D. Stur.—Ueber zwei neue Farne aus den Sotzka-Schichten von
Mottnig in Krain, 1 (2 plates).
H. Wolf.—Die Stadt-Oedenburg und ihre Umgebung, 15.
F. Foetterle-—Das Vorkommen, die Production und Circulation des
mineralischen Brennstoffs in der dsterreichisch-ungarischen Mo-
narchie im Jahre 1868, 65.
E. v. Mojsisovics.—Beitrage zur Kenntniss der Cephalopoden-Fauna
der ocnischen Gruppe, 98 (2 plates).
T. Fuchs und F. Karrer.—Geologische Studien in den Tertiarbil-
dungen des Wiener Beckens, 113 (1 plate).
K. v. Hauer.—Ueber den Kainit von Kalusz in Galizien, 141.
Sitzungsberichte der k.-k. Akademie der Wissenschaften in
Wien. Mathematisch-naturwissenschaftliche Classe. Band ly.
Abth.i. Hefte 1&2. June and July 1869.
G. Tschermak.—Mikvoskopische Unterscheidung der Mineralien aus
der Augit-, Amphibol- und Biotitgruppe, 5 (2 plates).
C. v. Ettingshausen.—Beitrage zur Kenntniss der Tertiarflora
Steiermarks, 17 (6 plates).
——. Band lvii. Abth. ii. Hefte 1 & 2. June
and July 1869.
G. Neumayer.—Bericht iiber das Niederfallen eines Meteorsteines
bei Krahenberg, Kanton Homburg, Pfalz, 229.
DONATIONS. 169
Vienna. Verhandlungen der k,-k. geologischen Reichsanstalt. 1870.
Nos. 12-14. . :
J. F. J. Schmidt.—Erdbeben in Griechenland, 226.
T. Herbich.—Hallstatter-Kalk in Ost-Siebenbiirgen, Stramberger-
Kalk bei Thoroczko, 227.
M. Adrian.—Erdbeben in Lissa, 228.
H. Wolf.—Aus den Gebieten des Deutsch-Banater und Serbisch-
Banater Grenz-Regimentes, 229.
E. vy. Mojsisovics.—Das Gebirge siidlich und dstlich yon Brixlege,
231.
D. Stur.—Ein neuer Fundort von Choristoceras Marshi, v. H., am
Gerstherge, im westlichen Gehange des Gaisberges bei Salzburg,
232.
F. Foetterle-—Der westliche Theil des serbisch-banater Militarerenz-
Gebietes, 253.
—. Die Gegend zwischen Turnu Severin, Tirgu Jiului und
Kraiova in der Kleinen Wallachei, 254.
F. vy. Richthofen.—Geologische Untersuchungen in China, 243.
J. Haast.—Geologische aus Neuseeland, 246.
F. Posepny.—Zur Genesis der Calmeilagerstatten, 247.
M. Neumayr.—Ueber die Identitat von Perisphinctes Greppini, Opp.
sp., und Per. oxrytychus, Neumayr, 249.
T. Fuchs.—Geologische Untersuchungen im Tertiarbecken yon Wien,
250.
E. Tietze.—Die Juraformation bei Bersaska im Banat, 254.
G. Stache.—Aus dem Zillerthale, 260.
E. Favre.—Der Moleson-Stock und die umgebenden Berge im Canton
Freiburg, 267.
C.L. Griesbach.—Briefliche Mittheilungen tiber Stid- und Ost-Afrika,
269.
T. Fuchs.—Die erzherzogliche Ziegelei in Wieselburg, 270.
A. E. Reuss.—Zwei neue Pseudomorphosen, 271.
K. Hofmann.—Das Kohlenbecken des Zsily (Schiel)-Thales, 271.
M. Neumayr.—Jura-Studien, 272.
D. Stur.—Vorkommen echter Steinkohle bei Steinberg unweit
Poltschach in Steiermark, 272.
F. Posepny’—Bemerkungen iiber die durch Herrn Ch. Moore ent-
deckte Petrefactenfiihrung der Erzginge N.W. Englands, 273.
K. Tietze.—Liassische Porphyre im stidlichen Banat, 275.
a aes Sand- und Lossgebiet der Umgegend von Jassenova,
ie
K. oem krystallinische Grundgebirge bei Bersaska im Banat,
280.
——. Die quaternaren Bildungen im siidlichen Banat, 280.
Wiesbaden. Jahrbiicher des Nassauischen Vereins fiir Naturkunde.
Jahrgang xxi. und xxii. 1867468.
M. OC. Grandjean.—Beitrag zur Kenntniss der Bildung fossiler Koh-
lenablagerungen, 383.
B. Kosmann.—Der Apatit von Offheim und der Kalkwavellit von
Dehrn und Ahlbach, 417.
170 DONATIONS.
II. PERIODICALS PURCHASED FOR THE LIBRARY.
Annals and Magazine of Natural History. Fourth Series. Vol. vi.
Nos. 34-36. October to December 1870.
H. A. Nicholson.—On the genus Clhimacograpsus ; with Notes on the
British Species of the genus, 370.
W. 8S. Kent.—On an existing Coral closely allied to the Palzozoic
genus Favosites; with remarks on the affinities of the Zubulata,
384 (2 plates).
S. V. Wood.—On Astarte excurrens and A. modesta, 423.
KE. D. Cope.—On the Reptilia of the Triassic formations of the
Atlantic region of the United States, 498.
Paleontographica: herausgegeben von Dr. W. Dunker und Dr. K.
A. Zittel. Vol. xvii. Part 6.
L. v. Heyden.—Fossile Dipteren aus der Braunkohle von Rott im
Siebengebirge, 237 (2 plates).
III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.
Abich, H. Apereu de mes Voyages en Transcaucasie en 1864. 8vo.
Moscou, 1865. Presented by Mrs. W, J. Hamilton.
Adams, C. B. Contributions to Conchology. Nos. 1,2,4—9. Pre-
sented by Mrs. W. J. Hamilton.
Description of forty-four supposed new Species and Varieties
of operculated Land-shells from Jamaica. 8vo. Amherst, 1849.
Presented by Mrs. W. J. Hamilton.
—-. Monograph of Stoastoma, a new Genus of new Operculated
Land-shells. 4to. Amherst, Massachusetts, 1849. Presented
by Mrs. W. J. Hamilton.
—. Monograph of Vitrinella, a new Genus of new Species of
Turbinide. Ato. Amherst, Massachusetts, 1850. Presented by
Mrs. W. J. Hamilton.
Adams, A. L. Outlines of the Geology of the Maltese Islands, and
Description of the Brachiopoda by Thos. Davidson. 8vo. 1864.
Presented by Mrs. W. J. Hamilton.
Agassiz, L. Glacial Phenomena in Maine. 8vo. Boston, 1867.
Presented by Mrs. W. J. Hamilton.
DONATIONS. 171
‘Amtlicher Bericht tiber die 29te Versammlung der Gesellschaft
deutscher Naturforscher und Aerzte zu Wiesbaden im September
1852. 8vo. Wiesbaden, 1853. Presented by Mrs. W. J. Hamilton.
Angas, G. F. Description d’Espéces nouvelles appartenant a plu-
sieurs Genres de Mollusques Nudibranches des Environs de Port
Jackson. Presented by Mrs. W. J. Hamilton.
Anonymous. Documents et Nouvelles Géographiques. Parts 1&2.
8yo. Paris, 1854-55. Presented by Mrs. W. J. Hamilton.
The Excavation of the Valleys of the Alps. 8vo. 1862.
Presented by Mrs. W. J. Hamilton.
Ansted, D. T. Facts and Suggestions concerning the Economic
Geology of India. 1. Coal-fields of India. 8vo. 1846. Pre-
sented by Mrs. W. J. Hamilton.
Description of Remarkable Mineral Veins. Presented by
Mrs. W. J. Hamilton.
Antiquités Antédiluviennes récemment trouvées en France et en
Angleterre. 8vo. 1859. Presented by W. Whitaker, Esq., F.G.S.
Archer, W. H. Abstracts of English and Colonial Patent Specifica-
tions relating to the Preservation of Food &c. 8vo. Melbourne,
1870.
. Patents and Patentees, from 1854 to 1866. 4to. Mel-
bourne, 1868.
Patents and Patentees. Vol.ii. Indexes for the year 1867.
4to. Melbourne, 1869.
- ——. Vol. iii. Indexes for the year 1868. 4to. Mel-
bourne, 1870.
——. Abstracts of Specifications of Patents applied for from 1854
to 1866: Acto Bu. 4to. Melbourne, 1870.
Austen, J. H. A Guide to the Geology of the Isle of Purbeck and
the south-west coast of Hampshire. 8vo. Blandford, 1852.
Presented by Mrs. W. J. Hamilton.
Bache, A. D. Report showing the Progress of the Coast Survey for
the year ending October 1847. Presented by Mrs. W. J. Hamilton.
Bamberg, Erster Bericht iiber das Bestehen und Wirken des natur-
forschenden Vereins zu. 1852. Presented by Mrs. W. J.
Hamilton.
Barrande, J. Dépdt organique dans les loges aériennes des Ortho-
ceres. S8vo. Paris, 1859. Presented by Mrs. W. J. Hamilton.
Baudon, A. Catalogue des Mollusques du Département de l’Oise.
8vo. Beauvais, 1853. Presented by Mrs. W. J. Hamilton.
172 _ _ DONATIONS.
Baylee, J. Moses, and his Misinterpreters: Geology, and her Mis-
interpreters: the Word of God, and its Infallible Truth. Pre-
sented by Mrs. W. J. Hamilton.
Bellefonds, L. de. Mémoire sur le Lac Moeris, présenté et lu 4 la_
Société Beyptienne le 3 Juillet, 1842. 4to. Alexandrie, 1843.
Presented by Mrs. W. J. Semele.
Beneden, P. J. van. La Cote d’Ostende et les Fouilles d’Anvers.
8vo. Bruxelles, 1862. Presented by Mrs. W. J. Hamilton.
Recherches sur les Squalodons. 4to. Bruxelles, 1865.
Presented by Mrs. W. J. Hamilton.
, et E. Dupont. Sur les Ossements Humains du Trou du
Frontal. Presented by Mrs. W. J. Hamilton.
Bertrand de Doue, J. M. Sur les Ossemens fossiles de Saint-Pri-
vant, et sur le terrain basaltique ou ils ont été découverts. Pre-
sented by Mrs. W. J. Hamilton.
Beyrich, E. Ueber den Zusammenhang der norddeutschen Ter-
tiirbildungen zur Erlauterung einer geologischen Uebersichtskarte.
4to. Berlin, 1857. Presented by Mrs. W. J. Hamilton.
Ueber die Lagerung der Kreideformation im schlesischen
Gebirge. 4to. Berlin, 1855. Presented by Mrs. W. J. Hamilton.
Ueber die Stellung der Hessischen Tertiirbildungen. 8vyo.
Berlin, 1854. Presented by Mrs. W. J. Hamilton.
Ueber ein Kohlenkalk-Fauna von Timor. 4to. Berlin, 1865.
_ Presented by Mrs. W. J. Hamilton.
Bianconi, J. J. Repertorio Italiano per la Storia Naturale. Reper-
torium Italicum, complectens Zoologiam, Mineralogiam, Geologiam
et Paleontologiam. 8vo. Bononie, 1853. Presented by Mrs.
W. J. Hamilton.
Bielz, E. A. Fauna der Land- und Susswasser-Mollusken Sieben-
burgens. 8vo. Hermannstadt, 1863. Presented by Mrs. W. J.
Hamilton.
Bigsby, J. J. On the Organic Contents of the Older Metamorphic
Rocks: a Review and a Classification. 8vo. Kdinburgh, 1863.
Presented by Mrs. W. J. Hamilton.
Blyth, E. Drafts for a Fauna Indica. Presented by Mrs. W. J.
Hamilton.
Bornemann, J.G. Ueber die Liasformation in der Umgegend von
Gottingen und ihre organischen Einschliisse. 8vo. Berlin, 1854,
Presented by Mrs. W..J. Hamilton.
Bosquet, J. Notice sur quelques Mollusques Lamellibranches Nou-
veaux. 8vo. 1851. Presented by Mrs. W. J. Hanulton.
fod
DONATIONS. 173
Bouchard-Chantereaux, M. Catalogue des Mollusques Marins obser-
vés jusqu’a ce jour a l’état vivant, sur les Cotés du Boulonnais.
Presented by Mrs. W. J. Hamilton.
Boucher de Perthes, J. De ?Homme Antédiluvien et ses Cuvres.
8vo. Paris, 1860. From W. Whitaker, Esq., F.GS.
Brodie, P. B. On the Geology of Warwickshire. 8vo. Warwick,
1870.
Practical Geology: Read in place of the Annual Address at
the winter meeting of the Warwickshire Naturalists’ Field-Club.
8vo. Warwick, 1869.
Buch, Leopold von. Gedechtniss-Rede. 4to. Berlin, 1853. Pre-
sented by Mrs. W. J. Hamilton.
Buckland, W. An Inquiry whether the sentence of death pro-
nounced at the fall of Man included the whole Animal Creation,
or was restricted to the Human Race. 8vo. 1839. Presented
by Mrs. W. J. Hamilton.
Buish,G. On the Physical Geography of Hindostan. 8vo. Edin-
burgh, 1854. Presented by Mrs. W. J. Hamilton.
Burnell, G. R. On the Influence of some external agents on the
durability of Building Materials. 4to. 1854. Presented by Mrs.
W. J. Hamilton.
Burr, F. Introduction to the Study of Geology. 8vo. 1836.
Presented by W. Whitaker, Esq., F.GS.
Capellini, G. Sui Testacei Marini delle Coste del Piemonte per J.
Gwyn Jeffreys, traduzione con note et un Catalogo speciale per il
Golfo della Spezia. 8vo. Genova, 1860. Presented by Mrs. W.
J. Hamilton.
Capellini, J., et O. Heer. Les Phyllites Crétacées du Nebraska.
4to. Zurich, 1866. Presented by Mrs. W. J. Hamilton.
Carega, F. Laurea in Scienze Naturali. 8vo. Pisa, 1853. Pre-
sented by Mrs. W. J. Hamilton.
Carpenter, W. B., J. Gwyn Jeffreys, and Wyville Thomson. Pre-
liminary Report on the Scientific Exploration of the Deep Sea in
H.M.S. ‘Porcupine.’ 8vo. 1870.
Catalogue of the Colonial Museum, Wellington, New Zealand. 12mo.
Wellington, 1870. Presented by the Colonial Museum, Wellington.
Catullo, A. Discorrimenti sopra alcuni importanti Fatti Geognos-
tico-Paleozoici. 8vo. Padova, 1865. Presented by Mrs. W. J.
Hamilton.
Chalmers, C. Notes for Inquiry. 8vo. 1855. Presented by Mrs.
W. J. Hamilton.
‘174 DONATIONS.
Chenu. Notice sur le Musée Conchyliologique de M. le Baron B.
Delessert. 8vo. Paris, 1849. Presented by Mrs. W. J. Hamilton.
Clark, W. . Observations on the Littorinide. Presented by Mrs. W.
J. Hamilton.
Cocchi, J. Sulla Geologia dell’ alta Valle di Magra. 4to. Milano,
1866. Presented by Mrs. W. J. Hamilton.
Cook, G. H. Geology of New Jersey. 8vo. Newark, 1868; and
Atlas. 4to. 1868.
Cotteau, G. Rapport sur les Progrés de la Géologie et de la Palé-
ontologie en France pendant V’année 1864. 8vo. Caen, 1865.
Presented by Mrs. W. J. Hamilton.
Rapport sur un Gisement de bois de cerfs, signalé par M.
Bavin aux environs de Guerchy (Yonne). Svo. 1864. Presented
by Mrs. W. J. Hamilton.
Rapport sur une Excursion Géologique dans les Terrains
Tertiaires et Quaternaires de l’Yonne et de la Cote-d@Or. 8vo.
1866. Presented by Mrs. W. J. Hamilton.
Crawfurd, J. A few Notes on Sir Charles Lyell’s ‘ Antiquity of
Man,’ and on Prof. T. H. Huxley’s ‘ Evidence as to Man’s Place
in Nature.’ 8vo. 1863. Presented by Mrs. W. J. Hamilton.
Croll, J. On Ocean-Currents. 8vo. 1870.
—. On the Cause of the Motion of Glaciers. S8vo. 1870.
Dana, J.D. Notes on the Eruption of Mauna Loa. 8vo. 1852.
Presented by Mrs. W. J. Hamilton.
Daubreée, A. Expériences sur la production artificielle de Apatite,
de la Topaze; et de quelques autres minéraux fluoriféres. Pre-
sented by Mrs. W. J. Hamilton.
Davidson, T. On Italian Tertiary Brachiopoda. Two Parts. 8vo.
1870.
Davis, J. E. Notes on Deep-sea Soundings. S8vo. 1867. Pre-
sented by Admiral Richards, Hydrographer to the Admiralty.
Dechen, H. von. Geognostische Beschreibung der Vulkanreihe der
Vorder-Kifel. S8vo. Bonn, 1861. Presented by Mrs. W. J.
Hamilton.
Geognostische Ucbersicht des Regierungs-Bezirks Ornsberg.
Presented by Mrs. W. J. Hamilton.
Delesse, A. Extraits de Minéralogie. 8vo. Paris, 1851. Pre-
sented by Mrs. W. J. Hamilton.
Sur le Gisement et sur Exploitation de |’Or en Australie.
8vo. Paris, 1853. Presented by Mrs. W. J. Hamilton.
DONATIONS. 175
Delesse, A. Mémoire sur la constitution minéralogique et chimique
des roches des Vosges. 8vo. Paris, 1850. Presented by Mrs.
W. J. Hamilton.
——. Idem. New edition. 8vo. Paris, 1853. Presented by
Mrs. W. J. Hamilton.
Untersuchungen tiber den rothen Porphyr der Alten und iiber
den rothen agyptischen Syenit. In’s Deutsche iibertragen von
G. Leonhard. 8vo. Stuttgart, 1852. Presented by Mrs. W. J.
Hamilton.
Delesse, H. Carte Lithologique de ’Embouchure de la Seine.
Deshayes, P. Conchyliologie de Vile de la Réunion (Bourbon). 8vo.
Paris, 1863. Presented by Mrs. W. J. Hamilton.
Dufrénoy. Rapport sur les Mines, les Opérations Métallurgiques, les
Produits Minéraux et les Carrieres, fait 4 la Commission Francais
du Jury International de l’Exposition Universelle de Londres.
8yo. Paris, 1854. Presented by Mrs. W. J. Hamilton.
Duncan, P. M. On the Madreporaria dredged up in the Expedition
of H.M.S. ‘Porcupine.’ 8vo. 1870.
Dunker, W. Ueber mehre Pflanzenreste aus dem Quadersandsteine
von Blankenburg. Presented by Mrs. W. J. Hamilton.
Egerton, P. G. A Systematic and Stratigraphical Catalogue of
Fossil Fish. 4to. 1837. Presented by Mrs. W. J. Hamilton.
Ettingshausen, C. von. Begriindung einiger neuen oder nicht genau
bekannten Arten der Lias- und der Oolithflora. Fol. Vienna,
1852. Presented by Mrs. W. J. Hamilton.
Beitrag zur Flora der Wealdenperiode. Fol. Vienna, 1852.
Presented by Mrs. W. J. Hamilton.
Beitrage zur fossilen Flora von Wildshuth in Oberdésterreich.
8yo. Vienna, 1852. Presented by Mrs. W. J. Hamilton.
Die Proteaceen der Vorwelt. Presented by Mrs. W. J.
Hamilton.
—. Ueber fossile Pandaneen. 8yvo. Vienna, 1852. Presented
by Mrs. W. J. Hamilton.
.. Ueber Palwobromelia, ein neues fossiles Pflanzengeschlecht.
Fol. Vienna, 1852. Presented by Mrs. W. J. Hamilton.
Evans, J. An address delivered in the Department of Ethnology
and Anthropology at the British Association. 8yvo. 1870.
Fischer, T. Verlags-Bericht. S8vo. Cassel, 1861. Presented by
Mrs. W. J. Hamilton.
176 DONATIONS.
Fitz-Roy, R. Considerations of the Great Isthmus of Central
America. Svo. 1850. Presented by Mrs. W. J. Hamilton.
Foetterle, F. Das Vorkommen, die Production und Circulation des
mineralischen Brennstoffes in der 6sterreichisch-ungarischen
Monarchie im Jahre 1868. 8vo. 1870.
Forbes, K. An Inaugural Lecture on Botany, read in King’s College,
London, 8th May, 1843. 8vo. 1843. Presented by Mrs. W. J.
Hamilton.
Report on the Investigation of British Marine Zoology by
means of the Dredge. 8vo. 1850. Presented by Mrs. W. J.
Hamilton.
Forbes, J. D. Account of his Recent Observations on Glaciers. Pre-
sented by Mrs. W. J. Hamilton.
—. Fourth letter on the Glacier Theory to Prof. Jameson. 8vo.
1842. Presented by Mrs. W. J. Hamilton.
Historical Remarks on the first Discovery of the Real Struc-
ture of Glacier-ice. Presented by Mrs. W. J. Hamilton.
Forchhammer, P. W. ‘Topographische und physiographische Be-
schreibung der Ebene von Troia. 4to. Frankfurt-am-Main,
1850. Presented by Mrs. W. J. Hamilton.
Fuchs, T., und F. Karrer. Geologische Studien in den Tertiirbil-
dungen des Wiener Beckens. 8vo. Vienna, 1870.
Geologische Karte von Preussen und den thiringischen Staaten.
Sheets Nos. 237-239 and 255-257; with Explanations and In-
troductory Remarks. From the Prussian Minister of Commerce
and Public Works.
Gerstfeldt, G. Ueber Land- und Stsswasser-Mollusken Sibiriens
und des Amur-Gebietes. 4to. St. Petersburg, 1859. Presented
by Mrs. W. J. Hamilton.
Giebel, C. Die Versteinerungen im Muschelkalk von Lieskau bei
Halle. 4to. Berlin, 1856. Presented by Mrs. W. J. Hamilton.
Gulliéron, V. Notice sur les Terrains Crétacés dans les Chaines
extérieures des Alpes des deux Cotes du Léman. 8yo. 1870.
Goeppert, H. R.. Sur la Structure de la Houille, Commentaire des
Photographies et des Exemplaires a |’Exposition Universelle de
Paris. Presented by Mrs. W. J. Hamilton.
Ueber ein im hiesigen konigl.-botanischen Garten zur
Erlaiuterung der Steinkohlen-Formation errichtetes Profil. 8yo.
Breslau, 1856. Presented by Mrs. W. J. Hamilton.
DONATIONS. 177
Goeppert, H. R., und F. Cohn. Bericht iiber die Thitigkeit der
naturwissenschaftlichen Section im Jahre 1853. 4to. Breslau,
1853. Presented by Mrs. W. J. Hamilton.
Goubert, E. Note sur le Gisement de Glos; suivie de la Description
des Fossiles du Coral-Rag de Glos, par Dr. K. Zittel et E. Gou-
bert. Presented by Mrs. W. J. Hamilton.
Gould, A. A. Expedition Shells; described for the work of the
United States Exploring Expedition, during the Years 1838-42.
8vo. Boston, 1846. Presented by Mrs. W. J. Hamilton.
Graells, P. Catalogo de los Moluscos Terrestres y de Agua Dulce
de Espana. 8vo. Madrid, 1846. Presented by Mrs. W. J.
Hamilton.
Griffith, R. An Address delivered at the Geological Society of
Dublin, 12th February, 1840. 8vo. Dublin, 1840. Presented
by Mrs. W. J. Hamilton.
Gysser, A. Die Mollusken-Fauna Baden’s. 8vo. Heidelberg, 1863.
Presented by Mrs. W. J. Hamilton.
Haulinger, W.von. Jubel-Erinnerungstage, Riickblick auf die Jahre
1845 bis 1870. 8vo. Wien, 1870.
Hamilton, C. W. Address delivered at the Anniversary Meeting of
the Geological Society of Dublin, 12th February, 1845. 8vo.
Dublin, 1845. Presented by Mrs. W. J. Hamilton.
Hamilton, W. J. Notes of a Journey in Asia Minor in 1837. 8vo.
1838. Presented by Mrs. W. J. Hamilton.
Hamilton, W. J., and H. E. Strickland. On the Geology of the
Western Part of Asia Minor. 4to. 1839. Presented by Mrs.
W. J. Hamilton.
Hauer, F. v. Der Goldbergbau von Vo6répatak in Siebenbirgen.
4to. Wien, 1851. Presented by Mrs. W. J. Hamilton.
——. Ueber die vom Herrn Bergrath W. Fuchs in den Venetianer
Alpen gesammelten Fossilien. Fol. Wien, 1850. Presented by
Mrs. W. J. Hamilton.
——. Ueber die Cephalopoden des Muschelmarmors von Bleiberg
in Karnthen. 4to. Wien, 1846. Presented by Mrs. W. J.
Hamilton.
Ueber neue Cephalopoden aus den Marmorschichten yon
Hallstatt und Aussee. 4to. Wien, 1849. Presented by Mrs.
W. J. Hamilton.
Haughton, S. Annual Address delivered before the Geological
Society of Dublin, 8th February, 1859. 8vo. Dublin, 1859.
Presented by Mrs. W. J. Hamilton.
VOL. XXVII.—PART I. N
178 DONATIONS.
Haughton, S. Notes on Irish Mines. No. 2. Lead-mines of Luga-
nure, county of Wicklow. 8vo. Dublin, 1855. Presented by
Mrs. W. J. Hamilton.
——. No.3. Mines of Kenmare, county of Kerry. 8vo.
abhi, 1855. Presented by Mrs. W. J. Hamilton.
On the Chemical Composition and Optical Properties of the
Mica of the Dublin, Wicklow, and Carlow Granites. 8vo. 1855.
Presented by Mrs. W. J. Hamilton.
On the Evidence afforded by Fossil Plants as to the Bound-
ary-line between the Devonian and Carboniferous Rocks. 8vyo.
Dublin, 1855. Presented by Mrs. W. J. Hamilton.
On the Iron-ores of Carnarvonshire. 8vo. Dublin, 1854.
Presented by Mrs. W. J. Hamilton.
On the Physical Structure of the Old Red Sandstone of the
county of Waterford, considered with relation to Cleavage, Joint-
surfaces, and Faults. 4to. 1858. Presented by Mrs. W. J.
Hamilton.
Hemans, G. W., and R. Hassard. On the future Water-supply of
London. 8vo. 1866. Presented by Mrs. W. J. Hamilton.
Héricart de Thury et Brongniart. Rapport fait 4 ’ Académie des
Sciences, sur un Mémoire relatif 4 la Géologie des environs de
Fréjus; par M. Ch. Texier. 8vo. Paris, 1833. Presented by
Mrs. W. J. Hamilton.
Hochstetter, F. von. Geologische Skizze von Gibraltar. 4to. Wien,
1857. Presented by Mrs. W. J. Hamilton.
Karlsbad, seine geognostischen Verhiltnisse und seine Quel-
len. 8yvo. Karlsbad, 1856. Presented by Mrs. W. J. Hamil-
ton.
Hopkins, W. On the Motion of Glaciers. 4to. Cambridge, 1844.
Presented by Mrs. W. J. Hamilton.
Hopkinson, J. On the Structure and Affinities of the Genus Diera-
nograptus. 8yo. 1870.
‘Howse, R. Supplemental Note on the Priority of the Tyneside 7
Catalogue, published August 17th, 1848. S8vo. 1859. Presented
by Mrs. W. J. Hamilton.
Hunt, R. On the Mines, Minerals, and Miners of the United
Kingdom. 8vo. 1865. Presented by Mrs. W. J. Hamilton.
Hunt, T. Sterry. Notes sur les Sources Acides et les Gypses du
Haut Canada. 4to. Paris, 1855. Presented by Mrs. W. J.
Hamilton.
DONATIONS. 179
Institute of Civil Engineers. The Education and Status of Civil
Engineers in the United Kingdom and in Foreign Countries.
Svo. 1870. From the Institution of Ciwil Engineers.
Jeffreys, J. Gwyn. Fourth Report on Dredging among the Shetland
Isles.. 8vo. 1867.
—. Mediterranean Mollusca. S8vo. 1870.
—. Norwegian Mollusca. 8vo. 1870.
Preliminary Report on the best Mode of Preventing the
Ravages of Veredo and other Animals in our Ships and Harbours.
8vo. 1861.
——-. Remarks on Mr. M‘Andrew’s ‘ Note on the Comparative Size
of Marine Mollusca in various Latitudes of the European Seas.’
8vo. 1860.
. Report of the Committee for Dredging on the North and
Kast Coasts of Scotland. 8vo. 1862.
——. Report on Dredging among the Channel Isles. 8vo. 1865.
-——. Notes on Swiss Mollusca. 8vo. 1855. Presented by Mrs.
W. J. Hamilton.
—. On the Marine Testacea of the Piedmontese Coast. 8vo.
1856. Presented by Mrs. W. J. Hamilton.
Report on Shetland Dredging. 8vo. 1865. Presented ‘by
Mrs. W. J. Hamilton.
Johnston, A. K. Historical Notice of the Progress of the Ordnance
Survey in Scotland. 8vo. Kdinburgh, 1851. Presented by Mrs.
W. J. Hamilton.
Jomard. Observations sur le Voyage au Darfour, suivies d’un
Vocabulaire de la Langue des Habitants et de Remarques sur le
Nil-Blanc Supérieur. 8vo. Paris, 1845. Presented by Mrs. W.
J. Hamilton.
Jones, T. R. On Ancient Water-fleas of the Ostracodous and. Phyl-
lopodous Tribes (Bivalved Entomostraca). 8vo. 1870.
Jukes, J. B. Additional Notes on the Grouping of the Rocks of
North Devon and West Somerset. S8vo. Dublin, 1867. Pre-
sented by Mrs. W. J. Hamilton.
Karrer, F. Ueber ein neues Vorkommen von oberer Kreideforma-
tion in Leitzersdorf bei Stockerau und deren Foraminiferenfauna.
8vo. Wien, 1870.
Kelly, J. Some Remarks on the Doctrine of Characteristic Fossils.
Svo. 1864. Presented by Mrs. W. J. Hamilton.
w 2
180 _DONATIONS.
Koenen, A. von. Ueber die Parallelisirung des norddeutschen, en-
glischen und franzosischen Oligocians. 8vo. 1867. Presented
by Mrs. W. J. Hamilton.
Ueber die Oligocin-Tertiirschichten der Magdeburger Ge-
gend. 8yo. 1863. Presented by Mrs. W. J. Hamilton.
Koninck, L. de. Discours sur les Progrés de la Paléontologie en
Belgique. Presented by Mrs. W. J. Hamilton.
——. Notice sur la Vie et les Travaux de P. L. C. E. Louyet.
12mo. Bruxelles, 1851. Presented by Mrs. W. J. Hamilton.
. Notice sur les Fossiles de l’Inde découverts par Dr. Fleming.
8vo. Liége, 1863. Presented by Mrs. W. J. Hamilton.
Krauss, Dr. Neue Kap’sche Mollusken, als Zusatz zu meiner Schrift
“die siidafrikanischen Mollusken.” Presented by Mrs. W. J.
Hamilton.
Lartet, E., et H. Christy. Cavernes du Périgord: Objets Gravés et
Sculptés des Temps Pré-Historiques dans Europe Occidentale.
8vo. Paris, 1864. Presented by Mrs. W. J. Hamilton.
Lawrence, W. An Introduction to Comparative Anatomy and Phy-
slology, being the two Introductory Lectures delivered at the
Royal College of Surgeons, 1816. 8vo. 1823. Presented by
Mrs. W. J. Hamilton.
Lea, H. C. Description of some new Fossil Shells from the Ter-
tiary of Petersbourg. 4to. Philadelphia, 1843. Presented by
Mrs. W. J. Hamilton.
Leonhard, G. Beitrage zur Geologie der Gegend um Heidelberg.
- 8vo. Heidelberg, 1844. Presented by Mrs. W. J. Hamilton.
——. Die Quarz-fiihrenden Porphyre. S8vo. Stuttgart, 1851.
Presented by Mrs. W. J. Hamilton.
Leonhard, K. C. v. Hiitten-Erzeugnisse als Stiitzpuncte geolo-
gischer Hypothesen. 8vo. Stuttgart, 1852. Presented by Mrs.
W. J. Hamilton.
Kiinstlicher Glimmer. (Kin Bruchstiick aus: Hutten-Er-
zeugnisse.) Presented by Mrs. W. J. Hamilton.
Linceo, G. P. Catalogo ragionato di una Collezione di Materiali da
Construzione. 4to. Roma, 1862. Presented by Mrs. W. J.
Hamilton.
Linnarsson, J. G. O. Om Vestergétlands Cambriska och Siluriska
Aflagringar. 4to. Stockholm, 1869.
Logan, W. E. Letter addressed to Mr. Joachim Barrande on the
Rocks of the Quebec Group at Point Levis. S8vo. Montreal,
1863. Presented by Mrs. W. J. Hamilton.
DONATIONS. 181
Lycett, J. On some new Species of Zrigonia from the Inferior
Oolite of the Cotteswolds, with Preliminary Remarks upon that
Genus. 8vo. 1853. Presented by Mrs. W. J. Hamilton.
Lyell, C. New York Industrial Exhibition Special Report. 4to.
1854. Presented by Mrs. W. J. Hamilton.
Observations on the Loamy Deposit called ‘ Loess” of the
Basin of the Rhine. 8vo. 1843. Presented by Mrs. W. J.
Hamilton.
Supplement to the Fifth Edition of a Manual of Elementary
Geology. Second edition. 8vo. 1859. Presented by Mrs. W.
J. Hamilton.
M‘Andrew, R. On the Geographical Distribution of Testaceous
Mollusca in the North Atlantic and neighbouring Seas. 8vo.
Liverpool, 1854. Presented by Mrs. W. J. Hamilton.
M‘Andrew, R., and Prof. E. Forbes. Notice of new or rare British
Animals observed during Cruises in 1845 and 1846. Presented
by Mrs. W. J. Hamilton.
Mackintosh, D. On the Nature, Correlation, and Mode of Accumu-
lation of the Dritt-Deposits of the West Riding of Yorkshire.
8vo. 1870.
Malm, A. W. Zoologiska Observationer. 2dra Hiiftet. 8vo.
Gothenborg, 1853. Presented by Mrs. W. J. Hamilton.
Marcou, J. Letter on some points of the Geology of Texas, New
Mexico, Kansas, and Nebraska; addressed to Messrs. F. B. Meek
and F.V. Hayden. S8vo. Zurich, 1858. Presented by Mrs. W.
J. Hamilton.
Martins, M. C., et B. Gastaldi. ssai sur les Terrains Superficiels
de la Vallée du Po, aux environs de Turin, comparés 4 ceux de
la Plaine Suisse. 8vo. Paris, 1850. Presented by Mrs. W. J.
Hamilton.
Meneghini, G. Laurea in Scienze Naturali conferita al Sig. Ales-
sandro Spagnolini. 8vo. Pisa, 1857. Presented by Mrs. W. J.
Hamilton.
Meyer, H. von. Ueber die Reptilien und Siugethiere der verschie-
denen Zeiten der Erde. 8vo. Frankfurt-am-Main, 1852. Pre-
sented by Mrs. W. J. Hamilton.
‘Migliarini, A. Osservazioni sopra i Numeri che usarono gli Etrus-
chi. 8vo. 1860. Presented by Mrs. W. J. Hamilton.
Mojsisovics, H.v. Beitrige zur Kenntniss der Cephalopodenfauna
der ocnischen Gruppe. 8vo. Wien, 1870.
182 DONATIONS.
Morris, J., and T. Rupert Jones. Geology. First Series. 8vo.
1870.
Mortillet, G. de. Histoire de la Savoie avant ’Homme. 8vo.
Annecy, 1856. Presented by Mrs. W. J. Hamilton.
Murchison, R. I. On the Relative Powers of Glaciers and Floating
Icebergs in Modifying the Surface of the Earth. 8vo. 1864.
Presented by Mrs. W. J. Hamilton.
Murchison, R. I., E. de Verneuil, and A. von Keyserling. On the
Geological Structure of the Central and Southern Regions of
Russia in Europe and of the Ural Mountains. S8yo. 1842.
Presented by Mrs. W. J. Hamilton.
Nardi, F. Sullo stato presente dei lavori pel taglio dell’ istmo di
Suez. 4to. 1867. Presented by Mrs. W. J. Hamilton.
Sulle bottiglie galleggianti come mezzo di esplorare le cor-
renti marittime. 4to. 1866. Presented by Mrs. W. J. Hamil-
ton.
Nardo,G. D. Sunto di aleune Osservazioni Anatomiche sull’ intima
struttura della cute de’ Pesci comparativamente considerata, e
sulle cause Fisiologiche e Fisico-Chimiche della loro colorazione
e decolorazione. 4to. Venezia, 1853. Presented by Mrs. W. J.
Hamilton.
Nasmyth, A. Report on a paper on the Cellular Structure of the
Ivory, Enamel, and Pulp of the Teeth, as well as of the Epithe-
lium &. 8yo. 1839. Presented by Mrs. W. J. Hamilton.
Nyst, H. Sur les Animaux Inférieurs Fossiles de la Province
d’Anvers. 8vo. Bruxelles, 1869.
Descriptions succinctes de dix espéces nouvelles de Coquilles
Fossiles du Crag noir des Environs d’Anvers. Presented by Mrs.
W. J. Hamilton.
Notice sur un nouveau Gite de Fossiles se rapportant aux
espéces Faluniennes du Midi de l’Europe, découverte 4 Edeghem
prés d’Anvers. Presented by Mrs. W. J. Hamilton.
Parfitt, EZ. Fossil Sponge-spicules in the Greensand of Haldon and
Blackdown. 8vo. 1870.
Pascuccit, Z. Brevi cenni sulle specialita Mattei con sunto delle
malattie sanate nella citta di Roma nell’ anno 1869. 8vo.
Roma, 1870.
Pessina, L. G. Quistioni Senmineln e Ricerche Meteorologiche. Svyo.
Firenze, 1870. ;
DONATIONS. 183
Pietet, F. J., et E. Renevier. Céphalopodes de Cheville. 8vo.
Lausanne et Paris, 1866. Presented by Mrs. W. J. Hamilton.
Ponzi, G. Societa in partecipazione per la Ricerca ed Escavazione
dei Carboni Fossili nel Territorio di Tolfa. Rapporto Scientifico
sui lavori eseguiti e sullo stato attuale delle Miniere. © 4to.
Roma, 1860. Presented by Mrs. W. J. Hamilton.
Portlock (Colonel). Continuation of a Memoir of the late Major-
General Colby. Presented by Mrs. W. J. Hamilton.
Prado, C. de. Vadeon, Cain, la Canal de Terea. Ascension a los
picos de Europa, en la cordillera Cantabrica. Presented by Mrs.
W. J. Hamilton. Fr
Prestwich, J. Mémoire sur la Position Géologique des Sables et du
Calcaire lacustre de Rilly (Marne). 8vo. Paris, 1853. Pre-
sented by Mrs. W. J. Hamilton.
——. On some New Facts in Relation to the Section of the Cliff
at Mundesley, Norfolk. 8vo. 1860. Presented by Mrs. W. J.
Hamilton.
On the Geological Position and Age of the Flint-implement
bearing Beds, and on the Loess of the South-east of England and
North-west of France. 4to. 1864. Presented by Mrs. W. J.
Hamulton.
On the Loess of the Valleys of the South of England, and
of the Somme and the Seine. 8vo. 1862. Presented by Mrs.
_W. J. Hamilton.
On the Occurrence of Flint Implements, associated with the
Remains of Extinct Mammalia, in undisturbed Beds of a late
Geological Period. 8vo. 1859. Presented by Mrs. W. J.
Hamilton.
Quentin, C. An Account of Paraguay; its History, People, and its
Government. 8yvo. 1865. Presented by Mrs. W. J. Hamilton.
Ramsay, A.C. Sir Charles Lyell and the Glacial Theory of Lake-
basins. 8vo. 1865. Presented by Mrs. W. J. Hamilton.
. The Excavation of the Valleys of the Alps. 8vo. 1862.
Presented by Mrs. W. J. Hamilton.
——. The Old Glaciers of Switzerland and North Wales. .8vo.
1859. Presented by Mrs. W. J. Hamilton.
Reeve, L. A Revision of the History, Synonymy, and Geographical
Distribution of the Recent Terebratule. Presented by Mrs. W. J.
Hamilton.
. On a new Species of Zymnea from Thibet. Presented by
Mrs. W. J. Hamilton.
184 DONATIONS.
Renevier, E. Description des Fossiles du Terrain Nummulitique
Supérieur des environs de Gap, des Diablerets, et de quelques
localités dela Savoie. 8vo. Grenoble, 1854. Presented by Mrs.
W. J. Hamilton.
Notices Géologiques et Paléontologiques sur les Alpes Vau-
doises. Svo. 1865. Presented by Mrs. W. J. Hamilton.
Notices Géologiques et Paléontologiques sur les Alpes Vau-
doises. III. Environs de Cheville. S8vo. Lausanne et Paris,
1866. Presented by Mrs. W. J. Hamilton.
Report. Annual Report of the Leeds Philosophical Society.
' 1869-70. From the Leeds Philosophical Society.
——. Annual Report of the State Geologist of New Jersey for
1869. 8vo. Trenton, N. J., 1870. Presented by Prof. G. H.
Cook.
Thirty-fourth Annual Report of the Warwickshire Natural-
History and Archeological Society. April 1870. rom the
Warwickshire Natural-History and Archeological Society.
of the Select Committee on the Geological Survey. 8vo.
Quebec, 1855. Presented by Mrs. W. J. Hamilton.
Richthofen, Baron von. Reports on the Provinces of Hunan, Hupeh,
Honan, and Shansi. 1870.
Robert, F. Mémoire sur les Ossemens Fossiles des environs de
Cussac. 8vo. Puy, 1830. Presented by Mrs. W. J. Hamilton.
Robinson, Dr. OnSoil. Newedition. 8vo. 1863. Presented by
Mrs. W. J. Hamilton.
Romer, E. Die Familien, Genera, Subgenera, und Sectionen der
zweimuskeligen kopflosen Mollusken. 4to. Cassel, 1863. Pre-
sented by Mrs. W. J. Hamilton.
Rossmiissler, E. A. Ueber eine Fauna molluscorum extramarinorum
Europe und einen Prodromus fiir eine solche. Presented by Mrs.
W. J. Hamilton.
Roth, J. Die Fortschritte der physikalischen Geographie im Jahre
1852, 1853, 1854 und 1857. Presented by Mrs. W. J. Hamilton.
Sandberger, F. Die Land- und Siisswasser-Conchylien der Vorwelt.
Folio. Wiesbaden, 1870.
——. Ueber Isoklas und Kollophan, zwei neue Phosphate. 8vo.
1870.
Beobachtungen in der Wutrzburger Trias. 8vo. 1864.
Verecucd by Mrs. W. J. Hamilton.
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Sandberger, F. Die Gliederung der Wiirzburger Trias und ihrer
Aiquivalente. Presented by Mrs. W. J. Hamilton.
——. Die Stellung der Raibler Schichten in dem frankischen und
schwiibischen Keuper. Presented by Mrs. W. J. Hamilton.
——. Nachtrigliche Bemerkungen zu meiner Abhandlung ther
Olivinfels. Svo. Wurzburg, 1866. Presented by Mrs. W. J.
Hamilton.
Zircon (Hyacinth) im Fichtelgebirge. S8vo. 1866. Pre-
sented by Mrs. W. J. Hamilton.
Sandberger,G. Beobachtungen tiber mehrere schwierigere Puncte der
Organisation der Goniatiten. Presented by Mrs. W. J. Hamilton.
Clymenia subnautilina (nova sp.) von Weilburg. 8vo.
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Paliontologische-geognostiche Kleinigkeiten aus den Rhein-
landen. Presented by Mrs. W. J. Hamilton.
Wesen und Bedeutung der Paliontologie. 12mo. Wies-
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baden, 1855. Presented by Mrs. W. J. Hamilton.
Santagata, D. Delle Metarhorfosi del Caleareo Compatto nel Bolog-
nese. 4to. Bologna, 1848. Presented by Mrs. W. J. Hamilton.
Sauvage, EK. Htudes sur le Terrain Quaternaire de Blandecques (Pas-
de-Calais). 8vo. 1865. Presented by W. Whitaker, Esq., F.G.S.
Les Grottes de la Basse-Falize prés Hydrequent. 8vo. 1866.
Presented by W. Whitaker, Esq., F.GS.
Scacchi, A. Catalogus Conchyliorum Regni Neapolitant. 8vyo.
1836. Presented by Mrs. W. J. Hamilton.
Scrope, G. P. On the Mode of Formation of Volcanic Cones and
Craters. 8vo. 1859. Presented by Mrs. W. J. Hamilton.
Sedgwick, A., and R. I. Murchison. Classification of the Older
Stratified Rocks of Devonshire and Cornwall. 8vo. 1839. Pre-
sented by Mrs. W. J. Hamilton.
Sedgwick, A. On the May-Hill Limestone, and the Paleozoic System
of England. 8vo. 1854. Presented by Mrs. W. J. Hamilton.
Seetzen. A brief Account of the Countries adjoining the Lake of
Tiberias, the Jordan, and the Dead Sea. 4to. Bath, 1810. Pre-
sented by Mrs. W. J. Hamilton.
Shortland, P. F. Sounding Voyage of Her Majesty’s Ship ‘ Hydra.’
8vo. 1869. Presented by Admiral Richards, Hydrographer to the
Admiralty. ‘
VOL. XXVII.—PART I. 0
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Smith, Titus. Lectures on Mineralogy; delivered on March 5th,
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1834. Presented by Mrs. W. J. Hamilton.
Sorby, H.C. On Slaty Cleavage as exhibited in the Devonian
Limestone of Devonshire. 8vo. 1856. Presented by Mrs. W.
J. Hamilton.
Sowerby, G. B. Description of three new Shells. Presented by
Mrs. W. J. Hamilton.
Squier, E.G. Honduras Interoceanic Railway, with Maps of the
Line and Ports, and an Appendix. 8vo. 1857. Presented by
Mrs. W. J. Hamilton.
Staring, W.C. H. Onmerkingen over het zanddiluvyium van Noord-
Duitschlands, Nederland en Belgié. 8vo. Amsterdam, 1865.
Presented by Mrs. W. J. Hamilion.
——. Over Oude Meer-Oeverbanken op Java. 8vo. Amsterdam,
1866. Presented by Mrs. W. J. Hamilton. 3
Strickland, H. E. On the Geology of the Thracian Bosphorus.
4to. 1836. Presented by Mrs. W. J. Hamilton.
Studer, B. Eroffnungsrede der 43**" Versammlung schweizerischer
Naturforscher in Bern. 8vo. 1858. Presented by Mrs. W. J.
Hamilton.
——. les Couches en Forme de C dans les Alpes. Presented by
Mrs. W. J. Hamilton.
Sveriges Geologiska Undersékning. Sheets Nos. 31 to 35; with
descriptions and Geological Map of Ostradal. rom the Greological
Survey of Sweden.
Tate, R. A List of the Irish Liassic Fossils, with Notes on the New
and Critical Species. Appendix I. 8vo. 1870.
——. On the Land and Freshwater Mollusca of Nicaragua.
. Additions to the List of Brachiopoda of the British Secondary
Rocks. 8vo. 1869.
Tchihatchef, P. de. L’Asie Mineure et Empire Ottoman. 8vo.
Paris, 1850. Presented by Mrs. W. J. Hamilton.
Terquem, O., et E. Jourdy. Note sur le terrain bathonien de la
Moselle et de la Meuse. 8vo. Paris, 1869. Presented by Ralph
Tate, Esq., F.GS.
Tiberi, N. Descrizione di alcuni nuovi Testacei viventi nel Mediter-
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Sur les espéces du genre Cassidaria, qui vivent dans la Medi-
terranée. 8yo. Paris, 1863. Presented by Mrs. W. J. Hamilton.
Sy
DONATIONS. 187
Thompson, W. Opening Address at the Joint Meeting of the Natural
History and Philosophical Society and the Naturalists’ Field-Club
at the Belfast Museum. 8vo.1869.
Tournouér. Notes Stratigraphiques et Paléontologiques sur les Faluns
du département dela Gironde. 8vo. Paris, 1862. Presented by
Mrs. W. J. Hamilton.
Tourrette, Dr. Memoir concerning the Acidulous, Gaseous, Bi-
carbonated Sodaic Waters of Vals. 8vo. Paris, 1866. Presented
by Mrs. W. J. Hamilton.
Uhde, C. Catalogue des Objects formant le Musée Aztéco-Mexicain.
8vo. Paris, 1857. Presented by Mrs. W. J. Hamilton.
Vaux, A. de. Etudes des moyens propres a soustraire les Ouvriers
Mineurs au danger d’Asphyxie 4 la suite des coups de feu.
Presented by Mrs. W. J. Hamualton.
Statistique. Mines, Miniéres, usines Minéralurgique et
Machines a Vapeur. Presented by Mrs. W. J. Hamilton.
Verneuil, E. de, et J. Barrande. Faune primordiale dans la Chaine
Cantabrique. Presented by Mrs. W. J. Hamilton.
Victoria. Reports of the Mining Surveyors and Registrars. Quarter
ending 30th June, 1870. From the Colonial Government, Victoria.
Villa, Ant. e Giov. Batt. Catalogo dei Molluschi della Lombardia.
S8vo. Milano, 1844. Presented by Mrs. W. J. Hamilton.
——, ——. Dispositio systematica Conchyliorum terrestrium et fiu-
viatilium. 8vo. Milan, 1841. Presented by Mrs. W. J. Hamilton.
Virlet, T. Notice surles Bitumes. Presented by Mrs. W. J. Hamilton.
Wallace, A. R. On the Rio Negro. 8vo. 1853. Presented by
Mrs. W. J. Hamilton.
Watson, R.S. The Villages around Metz. 8vo. Newcastle-upon-
Tyne, 1870.
Weaver, T. On the Older Stratified Rocks of North Devon, with
correlative remarks concerning Transition or Protozoic Regions
in general. Syo. 1839. Presented by Mrs. W. J. Hamilton.
Westall, E. On the Advantages to be derived from the Adoption
of the “ Local Government Act,” as exemplified in Croydon. 8vo.
1865. Presented by W. Whitaker, Esq., F.G.S.
Williamson, W. C. On the Minute Structure of the Calcareous
Shells of some Recent Species of Foraminifera. Presented by Mrs.
W. J. Hamilton.
Wiltshire, T. On the Ancient Flint-implements of Yorkshire and
the Modern Fabrication of similar Specimens. 8vo. 1862. Pre-
sented by Mrs. W. J. Hamilton.
188 DONATIONS.
Wood, 8, V.,jun. On the Belgian Equivalents of the Upper and
Lower Drift of the Eastern Counties. 8vo. 1864. Presented by
Mrs. W. J. Hamilton.
On the Formation of the River- and other Valleys of the East
of England. 8vo. 1864. Presented by Mrs. W. J. Hamilton.
On the Red Crag, and its Relation to the Fluvio-marine
Crag, and on the Drift of the Eastern Counties. 8vo. 1864.
Presented by Mrs. W. J. Hamilton.
Yates, J. On the Use of Bronze Celts in Military Operations. 8vyo.
1849. Presented by Mrs. W. J. Hamilton.
Zigno, A. de. Intorno di Cenni del Professore Tomaso Antonio
Catullo sopra il Sistema Cretaceo delle Alpi Venete. 8yo. Pa-
dova, 1846. Presented by Mrs. W. J. Hamilton.
-——. Nouvelles Observations sur les Terrains Crétacés des Alpes
Vénitiennes. 8vo. Padoue, 1850. Presented by Mrs. W. J.
Hamitton.
——. Sui Terreni Jurassici delle Alpi Venete e sulla Flora Fossile
che li distingue. 8vo. Padova, 1852. Presented by Mrs. W.
J. Hamilton.
Zirkel, F. Mikromineralogische Mittheilungen. 8vo. 1870.
Zittel, C. A. Denkschrift auf Christ. Erich Hermann yon Meyer.
4to. Miinchen, 1870.
——. Ueber den Brachial-Apparat bei einigen jurassischen Tere-
bratuliden und tiber einen neue Brachiopodengattung Dimerella.
TV. BOOKS &e. PURCHASED FOR THE LIBRARY.
Hall, H. Map of South Africa.
——. Map of the Eastern frontier of Cape Colony. 1856.
Landegrebe,G. Mineralogie der Vulcane. 8vo. Cassel und Leipzig,
1870.
Ooster, W. A,, und C. von Fischer. Protozoe Helvetica. Mit-
theilungen aus dem Berner Museum der Naturgeschichte iiber merk-
wiirdige Thier- und Pflanzenreste der schweizerischen Vorwelt.
Band II. Part 2. 1870:
Pictet, F. J. Matériaux pour la Paléontologie Suisse. Série y.
Livr. 9. 4to. Genéve et Bale, 1870. :
THE
QUARTERLY JOURNAL
OF
THE GEOLOGICAL SOCIETY OF LONDON.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
JANUARY 25, 1871.
Richard Atkinson Peacock, Esq., of St. Helier’s, Jersey ; Arthur
W. Waters, Esq., Davos Plaz, Canton of Grisons; R. Koma, Esq.,
of University College, London; and Ransom Franklin Humiston,
Esq., M.A., Professor of Chemistry in Cleveland University, U. S.,
were elected Fellows of the Society.
The following communications were read :—
1. On the Puystcat Retarions of the New Rep Mart, Ruzric Bens,
and Lower Lras. By Prof. A. C, Ramsay, LL.D., F.R.S., &e.
Tr we look upon the Rheetic beds of Europe as a whole, it is evident
that they were formed under very different conditions in different
areas. Thus this formation on the south side of the Alps, as
described by Stoppani, contains a large and well-developed marine
fauna, whereas in England, Germany, Sweden, and in other parts of
the north of Europe, the strata are much less developed, and the
fauna has dwindled, containing fewer forms of life, while most of
them are small and some distorted in appearance.
In this paper I propose to inquire into the reason of these pecu-
liarities with regard to the English beds, and to show their relations
to the New Red Marl and the Lower Lias in a physical point of
view.
I have for some years held that the New Red Marl is physically
more. intimately connected with the Rhetic beds, and, in some
respects, even with the Lower Lias, than it is with our own New
Red Sandstone. The absence of the Muschelkalk in England
probably attests a break in succession in our Triassic series. I say
probably, because the opinion is every day growing stronger that our
_ VOL, XXVII.—PART I. P
190 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
Triassic series was deposited in inland waters, partly fresh or salt as
the case may have been, whereas the continental Trias was partly, at
any rate, deposited in areas connected with the sea. If, between the
deposition of the New Red Sandstone and Marl in England, the
area in which they occur was not for a time depressed beneath
the sea, we have a sufficient reason for the absence of the Muschel-
kalk. There are, indeed, symptoms of a gap in time between
our Bunter and Keuper strata, accompanied by slight indications of
disturbance and unconformity ; and, at all events, there is in places
a very marked overlap of the Marl across the Bunter Sandstone
series.
In England there is a perfect physical gradation between the New
Red Marl and the Rheetic beds, shown by interstratifications of red,
green, and grey marls which, varying in different localities, pass by
degrees into limestones, sandstones, and black shales. It is therefore
impossible to determine precisely where the Rheetic beds commence
in this series; and, indeed, all through the New Red Marl there is
a tendency to a repetition of the same sort of deposits as those with
which the ordinarily recognized Rhetic beds were ushered in.
This is evinced by the frequent local recurrence of green and grey
marls, and thin beds of light-grey and whitish sandstones, commonly
called the Middle Keuper Sandstones, which, however, occur in many
horizons in the New Red Marl.
I have long held, in common with some other geologists, that
our New Red Sandstone was probably deposited in an inland lake,
and that our New Red Marl was ‘certainly formed in a salt lake*.
This belief is founded on the existence of the great deposits of rock-
salt common in that formation, on the ground that, such lakes being
fed by rivers and having no outflow, concentration of salts ensued
by evaporation, and saline deposits were at length formed, in this
case consisting chiefly of common salt. To me it seems impossible
that solid salt can be deposited in quantity in an ordinary ocean,
for the salt in solution cannot be sufficiently concentrated there to
permit of deposition. And though wide-spreading cakes of salt have
been formed by evaporation in such areas as the Runn of Cutch,
yet this seems rather to partake of the nature of an accident than to
denote a steady, long-continued train of events like those which
marked the deposition of salt in our Keuper series.
Gypsum and other salts accompanying the New Red Marl may
also have been formed in like manner ; and I consider that the per-
oxide of iron which stains both salt and marl may also have been
carried into the lakes in solution as carbonate of iron, and afterwards
deposited as a peroxide through the oxidizing action of the air and
the escape of the carbonic acid which held it in solution. I¢ is well
* As far as I know, first proposed by the late Professor H. D. Rogers. in an
address to the British Association at Glasgow, 1855, p. 5, “On some of the
Geological Functions of the Winds, illustrating the Origin of Salt.” Only the
title was printed ; but ever since I have adopted and expounded Professor Rogers's
views in my lectures. Mr. Moore mentions ‘the fresh- or brackish-water depo-
sits of the Upper Trias,” Quart. Journ. Geol. Soc. vol. xxiii. p. 458.
1871.] RAMSAY—LOWER LIAS. 191
known that the peroxide of iron, as a thin pellicle, only incrusts the
grains of sand that form the New Red and other red sandstones ;
and microscopic examination of the New Red Marl proves that
the grains or flakes of sandy mud composing it are encased in
the same manner*, Both Sandstones and Marls, I believe, have
been formed in lakes, and their red colour is connected with this
circumstance; for it seems impossible that an oxide of iron could
be deposited from solution in an open sea in sufficient quantity
to colour sediments red, though common pink mud might be so
formed from the mechanical waste of red granite or other rocks.
The remains of land-plants in the Keuper series, and the peculiarities
of some of the reptiles of the period, tend to confirm the view that the
strata were deposited in inland salt lakes. Their footprints prove
that they walked over moist surfaces ; and if these surfaces had been
simply left by a retiring tide, they would generally have been obli-
terated by the returning flood, in the manner that we see every day
on our own sandy shores. Itseems to me that the surfaces on which
we now find fossil footprints were probably rather left bare by the
summer evaporation of a lake; these surfaces were baked by the sun,
and the footprints hardened, so as to ensure their perpetuation, before
the rising waters brought by flooded muddy rivers again submerged
the low flat shores and deposited new beds of silt, just as they do at
the present day round the Dead Sea and the Salt Lake of Utah.
The Foraminifera of the Keuper Marls, which are numerous,
might just as well have lived in a salt lake as in the open seat;
and the same may be said of Hstheria minuta. The single fish
of our Lower Keuper Sandstone, Dipteronotus cyphus, will fall under
the same category. The Microlestes antiquus, which occurs in the
bone-beds of Stuttgart, andin the Red Marls of Watchet, in Somer-
setshire, according to Mr. Boyd Dawkins +, proves nothing except
that there was land in the vicinity.
* Mr. Ward, of the metallurgical laboratory, Jermyn-street, at my request
discharged the colour from fragments of New Red Sandstone and Marl by an
acid solution of protochloride of tin. Both became white. Under the micro-
scope the marl appeared as a very fine-grained sandstone composed of perfectly
white minute fragments of silica. In both the grains had evidently been simply
coated with a thin pellicle of peroxide of iron. In the sandstone the peroxide
of iron was 1-89 per cent.
t Species of Foraminifera are exceedingly variable in form; and many of
them have a long range in geological time. They are therefore of little value
in helping to the determination of stratigraphical horizons. It may be true, for
example, that if the Chalk were entirely composed of Foraminifera it might be
difficult to distinguish from deposits now forming in the Atlantic; but if these
Atlantic deposits were, like the Chalk, half consolidated, heaved up, and denuded,
geologists would not feel at a loss regarding their age. They would miss, in the
first place, all the genera of Cephalopoda characteristic of the Chalk, besides
numerous peculiar genera and species of Echinodermata, and, perhaps with one
exception, all the species of Brachiopoda common in the Chalk. Further, over
large areas, they would be apt to find Tertiary strata of various ages intercalated
between the Old and New Cretaceous beds, which would at once furnish a clue
to men experienced in field geology.
{ Mr. Dawkins considers that these strata belong to the Rheetic beds; but the
marine Rheetic fossils have not been found so low.
p2
192 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
I have already said that the New Red Marl of England is more
closely related physically to the Rheetic and, in some respects, to
the Liassic beds, than to the Bunter strata; and I will now state
the stratigraphical phenomena that have led me to form this
Opinion.
South and south-west of the Mendip Hills, the New Red Marl
and the Magnesian Conglomerates at its base lie directly on Car-
boniferous strata. The Rheetic beds and Lower Lias immediately
succeed these, the former lying conformably on, and generally
passing into the Red Marl by obyious gradations. On the north,
between the Mendip Hills and Tortworth, the Keuper Marls and
sandstones, with occasional Magnesian Conglomerates, also lie on
Carboniferous strata. North of Tortworth, as far as the Severn, the
Marl, very thin and without any Lower Keuper Sandstone, lies
directly on Silurian strata; and on the north side of the estuary it
lies indifferently on Old Red Sandstone and Carboniferous rocks.
Everywhere in these districts it is immediately succeeded by Rhetic
beds, which graduate downwards lithologically into the Marls; and
these Rheetic beds are invariably followed by true Lower Lias. The
same is the case north and north-west of Gloucester, where the
Keuper beds lie on Old Red Sandstone ; and on the east of this area
the upper Marls still pass into Rheetic beds regularly overlain by Lias
Clay. It is not till we come towards the south end of the Malvern
range, that Bunter Sandstones appear beneath the Marl. On the
east side of the Malvern and Abberley range, the Bunter beds are
thrown out of sight by a fault; but further north they come out in
full force, extending along the flanks of the Permian strata that
bound the Forest of Wyre, the Coalbrook Dale country, and the
South Staffordshire Coal-field, whence they stretch along the eastern
limits of North Wales, to the estuary of the Dee and the Mersey.
Thence the full Bunter series skirts the Lancashire, Cheshire,
and North Staffordshire Coal-fields, lying frequently on Permian
rocks, then passing eastward by Ashbourne towards Nottingham,
and along the flank of the Magnesian Limestone northward into
Yorkshire *.
East of South Staffordshire the case is different. Round the
Warwickshire Coal-field, the Keuper strata, where unfaulted, lie
directly either on Permian or Carboniferous beds, with one small
exception north of Atherstone, where Bunter pebble-beds appear
for about a mile. Some very thin Bunter beds appear on and round
the flanks of the Leicestershire Coal-field ; but generally the Lower
Keuper Sandstones lie directly upon Coal-measures; while further east,
round Charnwood Forest, the marl lies directly on Cambrian rocks ;
and the same is the case with respect to the igneous bosses that rise
through the marl further south.
Wherever the New Red Marl seems to attain its complete thick-
ness, it passes into Rheetic strata; and these are always succeeded by
Lower Lias, as far as the Rheetic beds have yet been observed. Obser-
* Sometimes the Bunter beds are cut out by faults for a space; but this does
not affect the general question.
1871.] RAMSAY—LOWEB LIAS. 193
vations, more or less perfect, confirm this, from the south-western
parts of England, northward to the shores of the Tees, all on the
direct outcrop between the common Lower Lias and the recognized
New Red Marl. Two outliers of Rheetic beds, formerly called Lower
Lias, also appear at Bagots Park and near Newborough, north-west
of Burton-on-Trent ; and I do not doubt that the same strata would
be found at the base of the outlier of Lias near Whitchurch, in
Shropshire, if the rocks of that country were not so much obscured
by glacial drift. In Cumberland, round Carlisle, at the mouth of the
Vale of Eden, a great tract of Permian strata is directly overlain by
Keuper Marls, which are succeeded by Lower Lias, though as yet no
Rheetic beds have been noted in that area, which is. also deeply
covered by glacial débris and other superficial deposits. In fact,
wherever the New Red Mar! goes, the Lias follows in apparent con-
formity ; and wherever the examination has been complete, the
Rheetic beds are found between them, while the Bunter beds, which,
were the series complete, would lie beneath the Marl, are often
absent, in which case the Marl rests on Permian or any other strata
of older date. The Liassic and Rheetic beds, therefore, appear to act
in conformity with the New Red Marl, and in connexion with it;
while the last seems to have in England less immediate stratigraph-
ical relation to the New Red Sandstone—a fact possibly connected
with the absence of the Muschelkalk in Britain.
Having reached this point of the argument, it is time to consider
the palzeontological part of the question, in relation to the probable
physical geography of the time.
In Stoppani’s descriptions of the Upper-Trias fossils of Esino * he
gives descriptions and figures of a magnificent suite of fossils from
beds which, according to his classification, ought to be the general
equivalents of our New Red Marl. Only one of these species,
Anatina precursor, passes into his infra-Lias or <Avicula-contorta
zone. The Lower St.-Cassian and Hallstatt beds, on the oppo-
site sides of the Tyrolese Alps, are believed by Hauer and Suess
to be the general equivalents of the Keuper strata of Germany,
France, and England, and, of course, of the beds of Esino. They
number from 600 to 800 species of fossils.
In Stoppani’s work on the infra-Lias and Avicula-contorta zone f
of Lombardy, descriptions and figures of about 75 genera and
200 species are given, consisting principally of Mollusca, with a
few Echinodermata, Sponges, &c. The fossils are very nearly quite
distinct from those of the upper half of his infra-Lias beds, and of our
English Lower Lias generally. The thickness of the strata de-
scribed, the variety and number of the Mollusca and other forms,
together with the luxuriant development and proportions of the
individual shells, point to the existence in that area, in the south
and east of Europe, and elsewhere of a broad open ocean, fitted for
the habitation of a large and flourishing fauna—very different in
these respects from the development of the British Rheetic beds,
whether we regard their thickness or the fossils they contain.
* Milan, 1858-60. + Milan, 1860-65.
194. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
According to lists prepared by Mr. Etheridge for publication in
a forthcoming work, the British species in undoubted Rheetic beds
may be summarized as follows, omitting the Sutton species. For
the substance of the remarks regarding affinities and distribution of
the species named I am also indebted to Mr. Etheridge.
Foraminifera, thirteen genera and twenty-seven species; Crust-
acea 2, viz. Tropifer levis from one of the bone-beds, and Hstherra
minuta, first known in the Keuper Sandstones; one Brachiopod,
Discina Townshendi, the only one known in our Rheetic strata. Of
the forms named in this list, Lima precursor somewhat resembles
L. punctata of the Lias ; Monotis decussata occurs at the very top of
the Rheetic beds in thin limestone bands, which some writers cou-
-sider to form the bottom of the Lower Lias. Ostrea fimbriata may
possibly be O. irregularis of the Lias ; but oysters are of little value
in such an inquiry. Pecten valoniensis, also a true Rheetic shell, is
avery variable form. Plicatula interstriata probably passes into
the Lower Lias. Anoplophora musculoides, another true Rheetie
shell, also occurs with Monotis decussata in the thin limestone bands
at the top, which some call Lias. Mytilus minutus occurs both in the
Rhetic and Lower Lias strata. All the Gasteropoda of the Rheetic
beds (not including the Sutton species) are peculiar to that forma-
tion ; and the same is the case with the fish. Of the Reptilia, Plesio-
saurus costatus, P. Hawkinsii, and P. trigonus are common to the
Rheetic beds and the base of the Lower Lias*. The occurrence of
Microlestes antiquus in the Keuper Marls is an accident, its remains
having been washed into the strata from the neighbouring landy. Of
the whole, not more than four species of shells at the most pass into
the Lias ; and probably this may even be restricted to two. The Sau-
rians have a longer range ; and this is very significant.
In this list I do not include the Sutton forms given in Mr.
Etheridge’s list, fourteen in all, one of which (Ostrea multicostata) is
also found in the Muschelkalk, and three of which (Pecten Etheridgz,
P. suttonensis, and Mytilus minutus) are also Lias species. Few or
none of the remaining forms occur associated with the shells of the
ordinary Rheetic areas. The Sutton beds lie unconformably on the
Carboniferous Limestone, and stratigraphically and lithologically are
inseparable from the ordinary Lias limestone. The corals, which
Dr. Duncan has examined, occur in small, irregular, broken layers,
or rather in occasional white tufaceous limestone patches, at the very
* Since this paper was written, I have been informed by Mr. William Sanders,
of Bristol, that he has obtained the centrum of an Jchthyosaurus of vast size ‘in
close contact with the thick bone-bed at Aust Passage,” apparently identical with
L. platyodon of the Lower Lias.
Tt The Mendip Hills and the highlands of South Wales have been recog-
nized as land while the Trias was being deposited, ever since 1846, if not earlier.
Sir H. De la Beche (‘‘ On the formation of the Rocks of South Wales and South-
west of England,” vol. i. p. 239 e7 seg., Mem. Geol. Surv. of Great Britain) con-
siders the dolomitic conglomerates “on the Mendip Hills, for instance,” “to
have been beaches among islands.” See also Ramsay, ‘ Denudation of S. Wales,’
&e. p. 318, Mr. Moore also adopts the island theory, “ Abnormal Secondary
Deposits,” Quart. Journ. Geol. Soc. 1867, vol. xxiii. p. 454.
1871.] RAMSAY—LOWER LIAS. 195
base of the Lias, often crusting the Carboniferous Limestone on
which it rests. It is so insignificant in quantity that a few perse-
vering paleontologists might almost carry it away bodily in their
bags ; and its manner of occurrence has always suggested to me
the idea that it was formed in hollows in the rocks, partly by eva-
poration, between high- and low-water mark. The corals some-
times grew on the Carboniferous Limestone ; and the whole by sub-
sidence was afterwards buried underneath the Lias. Mr. Bristow
remarks that this mode of formation explains the presence of galena
and chert in the tufa*. They have been derived from the Car-
boniferous Limestone on the land side of the deposit. West of
Bridgend, as far as Pyle, the Rheetic beds become sandstones, indi-
cating an approximation towards the margin and shallow water.
Sir Charles Lyell has remarked that “‘the sandstones and clay
of the Keuper resemble the deposits of estuaries and a shallow sea
near the land, and afford in the north-west of Germany, asin France
and England, but a scanty representation of the marine life of that
periody. As regards the scanty marine life, this is true. Mr.
Ktheridge, in his paper “ On the Rheetic or Avicula-contorta beds at
Garden Cliff” +, observes that the Rheetic beds of England and the
west and north of Europe, were deposited in shallow seas and in
estuaries.
With Sir Charles Lyell’s suggestion, as regards the estuarine
nature of the Keuper beds of England, I do not agree, while Mr.
Ktheridge seems to me to be right respecting the conditions under
which our Rheetic beds were formed. My reasons for this opinion are
chiefly founded on physical considerations, leading to the following
conclusions, which form the main object of this paper.
1. The Triassic epoch over a great part of what is now Europe was
essentially a terrestrial one; that is to say, the Trias areas of depo-
sition in part, and some of them altogether, were surrounded by
continental land. In the latter part of this epoch the Keuper marls
were deposited in the British isles in a great lake, fresh or brackish
at the beginning ; and the same was occasionally true of other areas
of northern Europe and its adjoining seas, which lakes were for the
most part destitute of outlets to the sea.
2. These lakes gradually got filled with sediments. By and by,
through change of amount of rainfall, or through increase of heat,
the lake or lakes ceased to have an outflow ; that is to say, evapora-
tion was equal to, or greater than, the influx of water.
3. By degrees, through evaporation, the water became salter ;
concentration of salt or salts in solution ensued; and precipitation
of rock salt was one of the results.
* T have examined the Sutton beds with Mr. Bristow, and have no doubt
that they are Lower Lias. See “On the Lower Lias or Lias-Conglomerate of a
part of Glamorganshire,” Bristow, Quart. Journ. Geol. Soc. 1867, vol. xxiii.
p- 199. See also Mr. Charles Moore, “On Abnormal Conditions of Secondary
Deposits,” Quart. Journ. Geol. Soc. 1867, vol. xxiii. p. 526. Mr. Moore decides
the Sutton beds to be of Lower Liassic age.
+ Elements of Geology.
¢ Proceedings of the Cotteswold Naturalists’ Field Club, vol. iii, 1865.
196 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25
4, Subsequently by increase of rainfall or decrease of heat, the
waters again comparatively freshened, but still remained salt, a fact
proved by the occurrence of pseudomorphous crystals of salt in sandy
layers interstratified with the marls, up to, and even in, the recog-
nized Rhetic strata. Gypsum also occurs above the bone-bed.
These circumstances may be accounted for by the close relation of
the Rheetic beds to the ordinary marly series. That Rheetic areas
got dried by temporary isolation seems certain; for sun-cracks
have been observed in the strata by Mr. Bristow, and also BSE AL bs
morphous crystals of salt.
5. During the deposition of the upper part of the Keuper marls,
overlaps took place of upper across lower strata. This would
necessarily take place in any deep wide lake-basin first half
drained by mere evaporation, and again, by a change of conditions,
gradually filled with water from which sediments were being depo-
sited across a broader area.
For example, were the rainfall of the area drained by the Jordan
to increase gradually, the basin of the Dead Sea would by degrees
fill with water, and successive deposits of sediment would gradually
everlap each other on the shelving slopes of the lake-basin in which
solid salts had previously been deposited. There are examples of
this kind of overlap in the New Red Marl of England, in Somerset,
Gloucester, Hereford, and Leicester shires.
6. In the British area, sinking of the district took place at or about
the time when the lake or lakes got nearly filled with sediment ; and
the same may have been the case in other European areas. A
partial influx of the sea took place over shallow bottoms; and the
marine life that accompanied it, and the deposits that ensued, to-
gether form the Rheetic beds of England. These marine forms
migrated from a true Rhetic ocean, in which the Lower St.-Cassian
and Hallstatt beds were deposited. If the Dead-Sea area, by increase
of rainfall, got filled up, and if depression of land took place so as to —
admit the waters of the Red Sea or Mediterranean, analogous
results would ensue; for a marine or estuarine fauna would be
superimposed in shallow water, on a set of strata containing salt in
certain lower deposits. The Dead Sea, like the Keuper, is singularly
destitute of remains of aquatic life.
Under these conditions, it is evident that the thin Rheetic beds
of North-western Europe might have been deposited in great part
in shallow seas and in estuaries, or in lagoons, or in occasional salt
lakes of small or great dimensions, separated from the sea by ac-
cidental changes in physical geography. Many years ago, while at
Lyme Regis, the late Professor Edward Forbes stated to me that the
fauna of the White Limestone, at that time called White Lias,
reminded him, in its assemblage of forms, of the fauna of the Caspian
Sea ; and this seems to be a case in point, though not in all respects
strictly analogous*. The fauna of the Caspian is very small in
* Mr. Moore, speaking of the “‘ White Lias,” considers that “ the general cha-
racter of the deposit is such as we might expect to find in a lagoon or inland sea
1871.] - RAMSAY—LOWER LIAS. 197
number of genera and species; and some of the forms are poor and
dwarfed. It is a north-sea fauna; and when the area was first
separated from the main ocean, it was first freshened by influx of
rivers, while it is now again becoming salter by evaporation. The
result is the poverty and dwarfing of the forms. In the Black Sea
there are misshapen or monstrous forms of Mollusca, stated by
Forbes to be due to the freshened state of the water. Both of these
cases, relating to what may be called continental seas, bear upon
the subject in question, especially since the Rhetic fauna of
England is also comparatively poor in genera and species, when com-
pared with the well-developed fauna of Lombardy and other parts
of the south and east of Europe.
I now come to adifficult point. It is undoubtedly true in England
that the Lower Lias follows the Rheetic beds wherever they go; and
though there are symptoms of erosion between them at Penarth and
at Curry Rivell, in Somerset*, yet the conformity is, on the whole, so
complete, that wherever we meet with the base of the Lower Lias
we look for the Rheetic beds below, and as yet we have not been dis-
appointed. The question then arises, how is it that the transition
in these areas from the Rhetic to the Liassic forms is so sudden?
It is hard to answer this question ; but it may perhaps be met. by an
analogous case. The estuarine and the lagoon beds of the Purbeck
and Wealden series commenced in the Oolitic epoch, and ended in
the Neocomian or Lower Cretaceous epoch; and the change be-
tween the life of the Oolitic and Neocomian and Cretaceous de-
posits is as great as, and insome respects greater than, that between
the Rheetic and Liassic strata; and though the Rhetic beds were not
deposited in fresh water, yet, like parts of the Purbeck series, I
believe they were formed in shallow water under brackish semi-
estuarine conditions which endured for a long period.
In conclusion, I may state that the same kind of reasoning, with
differences, applies more or less to other red-coloured and to some
calcareous strata of England,*including the Permian, Old Red Sand-
stone, and even the red Cambrian formation. This I hope to treat
ofin a subsequent memoir. If this idea is true, and if this kind of
work be carried out, it must have an important bearing on certain
departments of paleontology in a manner already partly indi-
cated by Professor Huxley, and it may throw much light on the
distribution of the various forms of animal and vegetable life in
time and space. Without it, we must still in great part continue
to regard the various formations very much as we might a pack of
in which the beds were being very tranquilly deposited ” (‘‘ Abnormal Secondary
Deposits,” Quart. Journ. Geol. Soc. 1867, vol. xxiii. p.470). See this memoir for
a great deal of valuable information on these and other deposits. See also
memoir by Dr. Wright “On the Avicula-contorta beds,’ Quart. Journ. Geol.
Soc. 1860, vol. xvi., and others.
* This kind of erosion was evidently not accompanied by marked uncon-
formity, the result of serious disturbance of the Rhztic beds before the deposi-
tion of the ordinary Lias. Estuarine or tidal sea-currents would have been
sufficient to produce it when the Lias-sea first came across a slowly sinking
area.
198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
cards arranged in order, 1, 2, 3, and so on up to Knave, Queen and
King ; so that by their marks we should always be able to mention
the cards above and below any given number, unless it happened
that one or more had been surreptitiously abstracted from their
places. The lacustrine, as distinguished from marine formations, do
not strictly follow this rule.
Discussron.
Mr. Eruerier thought the question of the nature of the Rheetic
beds was to a great extent paleontological. The main point in
connexion with them was as to how the British beds were to be con-
nected with those of the Lombardic and Middle European areas. It
certainly seemed probable that in this part of the world the con-
ditions of life were different, the deposits being much less in thick-
ness, and the fauna much diminished; and where represented at all
the shells occurred in a dwarfed and stunted form. The exact
horizon and nature of the Sutton beds had still to be determined.
Mr. Gopwry-Avsten believed that every mass of red sandstone
would ultimately be referred to either a brackish or freshwater
origin. A comparison of the ancient and present area of the Caspian
Sea would tend to remove any doubt that might remain on the mind
of geologists as to the possibility of the existence of such vast
internal seas as those which had to be called in to account for these
formations. He regretted that former observers had not attached
more importance to the duration and extent of those freshwater
conditions which were found so commonly to have prevailed between
the periods of deposit of the great marine formations. There was
another fact to be borne in mind, that even in existing lakes the
water at the one end was sometimes completely fresh, and at the
other end salt, each of course with a different fauna.
Prof. Rupert Jones said that although there were good grounds
for the lake-theory, something might be said for shallow seas. He
remarked that sulphate of lime was deposited from sea-water before
salt, that oxide of iron might originate from chloride of iron dif-
fused in water whether of lakes or seas, and that the hematites of
Permian age were probably deposited in the sea. He considered
that Foraminifera required great caution when used as criteria, as
the varietal forms giving the facies were of more importance than
the genera and species. The Hstherie were never marine, although
often occurring in plenty in temporary freshwater pools on the sea~
shore. In his monograph of Hstheria he had said much to substan-
tiate the notion that freshwater conditions often prevailed during
the formation of the Keuper. Both in the Old Red Sandstone of
the Baltic provinces and in the Lettenkohle and Keuper of Ger-
many, when Estheria comes in, Lingula dies out. The repeated set
of formations in the Permian and the Trias precludes their contem-
poraneity, as supposed by Messrs. Godwin-Austen and Marcou.
Mr. Baverman remarked that the Hallstatt beds which had been
cited as marine contained large deposits of rock-salt.
1871.] HULKE—REPTILIAN SKULL. 199
M. Marcov thought that the difficulties in regarding these beds
as of freshwater origin were greater than the author supposed. The
absence of fossils in gypsum, though almost universal, was not total.
He had himself seen three specimens of Trigonta in gypsum from
Stuttgart.
Mr. Tate mentioned the discovery by Mr. Burton of marine
fossils in the Red Marl, in one instance in combination with vege-
table remains. He commented on the sharp demarcation observable
in Ireland between the Rhetic beds and the marl below, whereas
it was almost impossible to separate them from the Lias above. He
doubted, however, whether the true relations of the Rhetic beds
were to be worked out in thiscountry. As to the fossils of the Sutton
Stone, they were all purely Liassic.
Mr. Burron stated that the fossils from the Red Marl came from
a spot about five miles from Retford, in the direction of Gains-
borough, but he had not seen them im situ. There are, however,
no Rheetic beds within some miles.
The Rey. Mr. Winwoon, in the absence of Mr. C. Moore, from ill
health, inquired whether the author regarded the White Lias as
Rheetic, or Liassic.
Prof. Ramsay, in reply, was quite willing to accept marine fossils
as coming from the Red Marl. The fact of Hstheria, a brackish or
freshwater form, occurring in certain bands was in favour of his
views; as he considered that at intervals the saltness of the water
in such a lake as he had suggested must have varied. He could not
accept the probability of oxide of iron having been deposited in a
large sea-area to such an extent as to colour the sands. All rocks
that could be proved to be of marine origin, even when they con-
tained iron, were not stained red unless by infiltration from above.
He pointed out that the old area of the Caspian was far larger than
the lake in which he had suggested that the New Red Marl had been
deposited. If, as was more than probable, there had been during
all geological time continental areas somewhat in the same positions
as those of the present day, there must have been large areas of
inland drainage in which some such deposits as those in question
must of necessity have been fcrmed.
2. Note on a Lance Reprimian Sxvuz from Brooxs, Istp or Wieut,
probably DinosavRian, and referable to the Genus Ievanopon.
By J. W. Hurxs, F.R.S., F.G.S.
[Puats XT.]
Ir is remarkable that so little is known of the skulls of the Wealden
Dinosauria, the more so as their other remains have been procured
in some abundance in the south-east of England and the Isle of Wight
during the fifty years which have elapsed since Dr. Mantell’s disco-
very of an Iguanodon’s tooth in the quarry near Cuckfield. Hypsi-
lophodon Foxw is, I believe, the only one the form and a great part
200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
of the structure of whose skull are known, and this only recently,
from the Rev. W. Fox’s unique specimen, first exhibited at the Meet-
ing of the British Association 1868, and described by Prof. Huxley
in the 26th vol. of our Journal. Of the skulls of Iguanodon Man-
telli and Megalosaurus Buckland, the only parts which have been
determined are incomplete mandibles and fragments of maxille.
The skull of Hyleosaurus is still, so far as I can learn, represented
by the single small fragment of the base imbedded, at the end of the
vertebral column, in the Tilgate-Forest slab, purchased by the British
Museum of the late Dr. Mantell, and figured by him in his ‘ Fossils
of the British Museum,’ and by Prof. Owen in the ‘ British Fossil
Reptilia ;’ and the skulls of Polacanthus Foxit, Pelorosawrus, the
Cetiosauri, and Streptospondyli are altogether unknown.
In August 1865 I saw in the Rev. W. Fox’s collection a fossil
which he had recently found in Brixton Bay. It was plainly a
splendid fragment of what before its mutilation had been a very
large skull. A strong impression of its reptilian nature, together
with its marked dissimilarity to the skulls of the other orders of this
class found in the same formation (Chelonia, Crocodilia, and Ptero-
sauria), led me to assign Mr. Fox’s skull to a Dinosaur; and its size
pointed to one of the largest, as Jguanodon Mantelli.
In September 1869 I myself obtained at Brooke (a locality not
far from where Mr. Fox discovered his skull, and one famous for the
large number of Dinosaurian remains it has furnished) the hinder
part of a skull, which repeated the principal features of that which
I had seen in 1865 in Mr. Fox’s collection, and which also supplied
several parts wanting in his, particularly the occipital condyle,
proving my impression of the reptilian nature of his skull to have
been well founded.
Knowing Prof. Huxley to have been recently engaged on the
osteology of the Dinosauria, I showed him my prize soon after my
return to London; and he confirmed my opinion of its probably
Dinosaurian nature. A paper upon it from him would have been
so valuable that it would have given me the greatest pleasure to
have left its description in his hands; but his many and increasing
engagements have not allowed this; and, unwilling to withhold any
longer from fellow-workers what, I believe, is a distinct addition to
the craniology of this interesting order, I now venture myself to
bring the skull under your notice. In doing this I am happy to
acknowledge my obligations to Prof. Huxley for assistance as valu-
able as it has been kindly rendered.
The specimen consists of the nearly perfect cranium proper, the
facial segment having been broken off across the orbits. The freedom
of its outer surface from matrix, its polish, the smoothness of the
once rough fractured edges, and the presence of many recent Serpule
upon it show that it had been during a long time lying exposed in
the sea before it was thrown upon the shore.
Seen from above (PI. XI. fig. 3), its outlines are roughly like those
of an hourglass, owing to the strong incurve of the temporal regions.
The deep temporal fossz are bounded in front by massive postorbital
1871.] HULKE—REPTILIAN SKULL. 201
processes. These in their present abraded state are obtuse four-sided
pyramids, the lower side of which looks downwards, and contributed to
form the orbit ; another side looks backwards, and belongs to the tem-
poral fossa ; a third is directed upwards, and forms part of the sinci-
put; and the fourth, directed forwards, is part of the fractured surface
left by the separation of the facial segment of the skull. Behind, the
temporal fossz are limited by the outer and anterior surface of strong,
trihedral, divergent, suspensorial processes (sp) directed outwards
and backwards, from which the quadrate bones depended. The roof
of the skull in front is broad and transversely convex, and above the
middle of the temporal fossee it contracts so much that here it might be
properly described as crested (pa), the sides sloping almost vertically
from the mid ridge, with only a slight outward inclination, as low as
a horizontal groove running from front to back along the temporal
fossa, and marking, perhaps, the meeting of the lower border of the
parietal bone with those forming the side-walls of the skull. Behind,
the narrow crested part of the roof forks and sends outwards and
backwards the usual divergent parietal processes of lacertilian skulls.
An obscure serrated transverse line about °5 inch behind where the
facial segment has broken away is, perhaps, the suture between the
parietal and principal frontal bone. No parietal foramen is discern-
ible. That part of the parietal bone which roofs the front of the
cranial cavity is very dense; it attains a thickness of -9 inch. The
hinder part of the roof is even thicker, but it is much less solid and
consists principally of cancellous tissue.
Viewed from behind (fig. 4), the outline of the skull is an inverted
triangle. The left suspensorial process, forming the upper and outer
angle, on this side"is wanting; and the end of the right one (sp) is
abraded. On the right side the whole of the surface above the fora-
men magnum is much splintered; but the splinters having become
reunited with very little displacement, its form is not much changed.
When the floor of the cranial cavity is horizontal, the part of the occi-
pital surface immediately above the level of the foramen magnum looks
downwards and backwards, while the greater part of the surface above
this looks upwards and backwards, and it makes now an obtuse angle
with the sinciput ; but as the meeting line of the occiput and sinciput
is somewhat crushed in and worn, the angle may originally have been
much smaller. This incrushing has been favoured by the presence
here of the cancellous tissue already mentioned. The foramen mag-
num (f) is subcordate (in the language of botanists). Its vertical
diameter is 1-4 inch, and its transverse one 1:Ginch. Directly above
the foramen is a slight mesial swelling, from which a low horizontal
ridge is produced outwards. Laterally, below this ridge the surface is
gently hollow. The occipital condyle (ot) roughly resembles a horse-
shoe. Its upper surface is deeply grooved. Its transverse slightly
exceeds its vertical diameter. It projects considerably behind the
general plane of the occiput; and below, at the under surface of the
skull, a deep constriction separates it from the parts immediately in
front, making it nearly pedunculated.
The base of the skull (fig. 5) offers an extremely irregular surface.
202 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
In the middle line, from behind forwards, the basicranial axis exhibits
first the under surface of the occipital condyle (ot), which is followed
by a constriction -8 long, just mentioned. ‘To this succeed a pair of
large, blunt, conical swellings (6s), the obtuse summits of which point
downwards, outwards, and backwards. They are extensions of the
basisphenoid, and they form with the condyle three points on which
the skull rests when its base is placed on a flat table, in which posi-
tion the floor of the cranial cavity is nearly parallel with the plane
in which the points lie. Behind, a deep narrow cleft separates the
right and left basisphenoidal swellings ; in front they join and toge-
ther form a triangular base, from the front of which ascends a pro-
jecting four-sided rod (bps), three sides of which are seen at the under
surface of the skull, while the fourth is within (in the floor of the
cranial cavity). This rod measures at the under surface of the skull
3°9 inches long. It rises obliquely forwards, making with the floor
of the cranial cavity an angle of about 40°. Its under surface behind
is nearly 1-2 inch broad; it tapers slightly forward, so that at the
distance of 2 inches it has diminished °3 inch. Rather more than
the posterior half of this surface of the rod is hollow longitudinally
and transversely. In front the hollow contracts, and is followed by
a median ridge, of which the base only remains. From the begin-
ning of this ridge forwards the rod rapidly narrows; and here the
lower border is fractured, making it probable that there was a thin
onward production of bone between the orbits.
Along the sides of this axial rod are arterial and nerve-foramina.
The first and second pair of these, reckoned from behind (¢, ¢’), are
respectively the posterior and anterior apertures of a right and left
canal tunnelling the basisphenoid and crossing the bottom of the
hypophysial fossa, which is the course taken by the internal carotid
artery inreptiles. The third pair of foramina (11) are the outlets of
two short canals passing forwards and outwards from a transverse
depression in the floor of the cranial cavity, situated directly in front
of a low transverse ridge, which has the same relation to the hypo-
physial fossa that the tuberculum has to the sella turcica in the
human skull. This transverse depression corresponds, then, to that
which in the human skull lodges the optic commissure, and doubtless
here subserved the same purpose, the canals continued from it trans-
mitting the optic nerves to the orbit. It follows that the front half
of the ascending part of the basicranial axis as it lies between the
optic nerves and in front of the tuberculum sellz contains the pre-
sphenoid, the hinder half consisting of the basisphenoid. No traces
of the junction of the presphenoid and basisphenoid, nor of this with
the basioccipital, are discernible in a longitudinal section of the skull ;
the sutures which once existed between these originally separate
bones have completely disappeared.
At each side of the presphenoid, above the optic canals, in the
under surface of the skull is a smooth triangular space, the upper sur-
face of which contributes to form the flat floor of the anterior fossa
of the cranial cavity. Its relations show it to be the orbito-sphenoid
(fig. 2, os). The hinder border of that part of it appearing at the
1871.4 HULKE—REPTILIAN SKULL. 208
under surface of the skull is bounded by a raised broken edge directed
downwards and backwards from the postorbital process towards the
basisphenoid. The middle of this edge is crossed by a deep, narrow,
horizontal groove continued forwards from a large foramen (v) situ-
ated nearly Linch behind. This groove may have lodged the ramus
ophthalmicus of the 5th cranial nerve. All that part of the broken
edge which is above and external to this groove is narrow; it seems
to be the remains of the thin bony plate separating the orbit from
the temporal fossa; while below and internal to the groove the edge
widens into a broad, rough, four-sided mass having mesially and
inferiorly the ascending basisphenoidal rod, in front the smooth under
surface of the orbito-sphenoid, above the narrow groove for the
ophthalmic branch of the 5th nerve, and behind a wide, shallow,
vertical groove which descends from the large foramen lately men-
tioned. This latter, from its great size and its position, can be none
other than the aperture which transmits the 5th nerve, the mandi-
bular division of which was probably lodged in the wide shallow
groove descending from it. That part of the side wall of the skull
which lies in front of this foramen for the 5th nerve, behind the
orbito-sphenoid, and which below joins the basisphenoid, must con-
tain the alisphenoid. A narrow channel which ascends immediately
behind the wide shallow groove for the mandibular nerve from near
the posterior orifice of the carotid canal, and ends in a couple of
small foramina nearly at the level of the floor of the cranial cavity, is
probably arterial. One inch behind the foramen for the 5th nerve,
and at the same level, but separated from it by a buttress, is a de-
pression, at the bottom of which are two openings (fig. 1, v1). These
I take to be the auditory fenestre ; and if this view be right, the part
of the side wall in front of them, and behind the foramen for the
5th nerve, contains the prootic bone; while behind the auditory
fenestre a buttress ascending from the basis cranii towards the lower
border of the suspensorium for the quadrate bone, in front of the ex-
occipital, has the relations of the opisthotic. Ina triangular hollow
between this and the exoccipital are the foramina for the 8th and 9th
nerves (VII, IX).
The side walls of the skull behind the foramen for the fifth nerve,
corresponding to the hinder half of the temporal fossa, slope outwards
more than in front ; they project beyond the auditory fenestra, which
they overhang, after the manner of the eaves of a house; and be-
neath the overhanging eave, and nearly parallel with its outer border,
is a wide shallow groove produced from the hollow containing the
auditory fenestre horizontally backwards and outwards to the root
of the suspensorial process, which probably lodged the stapes.
The cranial cavity (fig. 2) is long and narrow. Its greatest trans-
verse measurement is in front ; and its maximum vertical one is at the
middle, nearly above the foramen for the fifth nerve. Two rather
broad constrictions divide it into three fossee. Of these the anterior
doubtless lodged the cerebral hemispheres; it opens below into a
remarkably large hypophysial pit (pf). The posterior wall of this
pit is vertical; it makes a right angle with the floor of the cranial
204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
cavity, while the anterior wall slants obliquely forwards. The
middle fossa, which is loftier than the anterior, is wider above than
below. Assuming it to have lodged the cerebellum and optic
tubercles, these dimensions point to a high location of the latter,
their position in the reptilian brain. The posterior fossa is the
smallest, it has a laterally compressed subcylindrical shape.
It must be borne in mind that in Reptiles we can only approxi-
mately deduce the form of the brain from that of the cranial cavity,
because, although in this class the brain fills the cranial cavity less
incompletely than it does in fish, in which a large interspace exists
between the surface of the brain and that of the cranial cavity, yet
there is nothing like the coaptation of the brain and its containing
chamber which occurs in the higher Vertebrata.
From the foregoing details it will have become apparent that the
most striking characteristics of the Wealden skull are :—1, the com-
pleteness of the bony brain-case ; 2, the obliteration of the sutures,
particularly those of the basicranial axis; 3, its massiveness; 4,
the great downward extension of the basisphenoid, with the at-
tendant upward slant of the lower border of the basi-presphenoidal
rod.
The completeness of the bony brain-case is an almost unique
feature in a reptilian skull, being known only in one other genus,
Dicynodon. In all other Reptiles the side walls and front of the
cranium in advance of the periotic bones are membranous, the ali-
and orbito-sphenoid, when present, being rudimentary*. But in this
skull well ossified and completely developed ali- and orbito-sphenoids
with a presphenoid fill this large space, which in other reptiles remains
membranous. The lesser membranous space present between the
supraoccipital and parietal bones in some lacertilian skulls (I am not
certain whether there is not an indication of it in Dicynodon) is
also absent from this.
Scarcely less remarkable in a reptilian skull is the disappearance
of the sutures, particularly those in the basicranial axis, the rule
being that in reptiles the primitive distinctness of the cranial elements
persists throughout life. To this rule only two other exceptions are
known to me: one of these is the similar skull in Mr. Fox’s collec-
tion, to which I have referred in the early part of this paper; the
other is the singular ornithocephalic reptilian skull discovered by
Dr. E. Bunzel, a short description of which was communicated to
us last session through Prof. Huxley, who kindly afforded me an
opportunity of seeing the original MS. and drawings.
In both these respects (the completeness of the bony brain-case
and the disappearance of the sutures) this skull departs from the
reptilian type and resembles the ornithic, which is characterized by
early obliteration of the sutures and complete ossification. The
curious upward slant of the part of the basi-presphenoidal rod visible
at the under surface of the skull seemed at first sight to be another
ornithic resemblance, the lower edge of the interorbital septum in
* In snakes the side walls of the cranium in front of the periotic bones are
formed of downward extensions of the parietal and frontal bones.
1871. | HULKE— REPTILIAN SKULL. - 205
Pelecanus having a similar upward slant; but a closer inspection
shows that the likeness is not a real one; for in Pelecanus the free
lower border of the septum, and the floor of the overlying cranial fossa
are nearly parallel, the basicranial axis is bent, the front half of it
making a large angle with the hinder half of it, while in this
Wealden skull the floor of the cranial cavity is nearly straight in its
entire extent, and the apparent inclination of the front half of the
basicranial axis is caused by the great downward production of the
basisphenoidal swellings behind and the bevelling off of the under
surface of the basi-presphenoid in front, with a corresponding
decrease of its vertical depth forward.
I have already stated my reasons for referring Mr. Fox’s skull,
and therefore mine, to a Dinosaur; assuming that this opinion is
accepted, it remains for me to submit the considerations which
lead me to refer it to an Jguanodon. I purposely use the indefinite
article, because Jguanodon is commonly spoken of as if the genus
had only one representative, 7. Mantelli, although the mandibles
and also the vertebre referred to this present variations which make
the existence of several species very probable. I wish, however,
my reference of the skull to the genus Zguanodon to be regarded
rather as an attempt awaiting confirmation or correction whenever
new and better material for the purpose is discovered. The jaws
and teeth, either of which would have determined the reference at
once, are lost; and the circumstances of the discovery of the skull
deprive us of the presumptive evidence of its nature which its
association with other bones might have afforded ; so that in seeking
for a clue by which to connect it with a particular Dinosaur we are
limited to what inferences may be drawn from its gisement, and to
what we can learn from the intrinsic features of the skull itself.
As regards the former, the bed from which it came cannot be as-
certained ; but we know that the locality is rich in remains of
Iguanodon : and with respect to the latter we find the clue, I think, in
the obliteration of the sutures ; for these have also appeared to me to
be effaced in several mandibles of Zguanodon which I have examined.
The loss of the articular end observable in all these has been
occasioned by a fracture across the mandible, and not by the disso-
lution of a sutural union. This is plainly the case in the largest man-
dible figured by Prof. Owen in his ‘ British Fossil Reptilia ;’ and three
reptilian mandibular articular bones in the Rev. Mr. Fox’s collec-
tion, probably of Jqguanodon, also clearly illustrate this. In other
Dinosaurian skulls, or portions of skulls, examined with especial
reference to this point, I have found the sutures persistent. They
are so in Hypsilophodon Foxti, from which this skull is also distin-
guished by its large size; they persist too in Scelidosaurus Harrisonit,
of the Lias, and in the Triassic Belodon’s skull. Whether they
persisted or not in Megalosaurus is doubtful; the maxilla, described
last session by Prof. Huxley, is not conclusive on this point; but a
maxilla of the allied Teratosaurus, preserved in the British Museum,
proves their persistence in this Saurian. The relative infrequency
of Megalosaurian remains in the Isle of Wight (I state this on the
VOL. XXVII.—PART I. Q
206 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 25,
authority of a verbal communication from Mr. Fox) renders it less
probable that the skull belonged to this Dinosaur than to an Jguano-
don. In the ornithocephalic skull of Struthiosaurus, Bunzel, the
sutures also disappear; but its broad rounded occiput, its large
downward slanting paroccipital processes (shown in the figures ac-
companying Dr. Bunzel’s description), and the absence of the basi-
sphenoidal swellings so conspicuous in my Wealden skull completely
distinguish it from this.
EXPLANATION OF PLATE XI.
Supposed skull of Iguanodon, from Brooke, Isle of Wight.
Fig. 1. View of right side of the skull.
Fig. 2. View of interior of the same. ‘
Fig. 3. View of upper surface of the skull.
Fig. 4. View of posterior surface.
Fig. 5. View of under surface: pa, parietal crest ; 7, temporal fossa; sp, suspen-
sorial process; o¢, occipital tuberosity; bs, basisphenoid ; bps, basi-
presphenoid ; 0s, orbitosphenoid ; pf, hypophysial fossa; f, foramen
magnum ; ¢, posterior opening of carotid canal; c’, anterior opening
of same; II, V, Vil, Vill, 1x, foramina of the respective pairs of nerves.
Discussion.
Prof. Huxtry congratulated the Society on the progress being
made in our knowledge of this interesting group of Reptiles and of
their ornithic affinities.
Mr. Srrtry remarked on the similarity of the internal cavity of
the skull to that of Ichthyosourus. Some of the external charac-
teristics differed much from what he was acquainted with in other
Dinosaurian skulls, which, in the base of the skull, more closely re-
sembled those of ordinary lizards. He considered that the affinities
of Dinosaurs hitherto demonstrated were in the direction of Teleo-
saurus, from which the position of what were supposed to be the
optic lobes in this skull materially differed in being more reptilian.
On the whole, from its want of similarity to Hypsilophodon, he was
not prepared to accept this skull as that of an Iguanodon, and
thought that scme doubt attached to its affiliation with the
Dinosaurs.
Mr. Hutxz briefly replied, and observed that he had limited his
speculations to those which legitimately arose from the facts before
him.
DeWilde lith
SKULL FROM BR
{
JOKE
Quart.Journ. Geol. Soc.Vol.XXVII. P1X! .
M.&NHanhart imp.
1871.] JUDD—PUNFIELD FORMATION. 207
Fepsruary 8, 1871.
The following communications were read :—
1. On the Puxrierp Formation. By Joun W. Jupp, Esq., F.G.S.,
of the Geological Survey of England.
ConTENTs.
I. Introduction.
II. Bibliography of the subject.
III. Sections in the Isle of Purbeck.
1. Punfield Cove.
2. Worborrow Bay.
3. Mewps Bay.
4, Lulworth Cove.
TV. Sections in the Isle of Wight.
1. Brixton Bay.
2. Compton Bay.
3. Sandown Bay.
V. Sections in the Weald of Sussex, Surrey, and Kent.
1. Leith Hill, near Guildford.
2. Hythe.
VI. Relations of the Punfield Formation to the Wealden, Neocomian, and
Cretaceous of the south of England.
1. Unconformity between the Cretaceous and Neocomian.
2. Variation in character of the Cretaceous, in proceeding from
east to west.
3. Thinning-out westward of the Neocomian and Wealden.
4. Relation of the Purbeck to the Wealden.
VII. Foreign equivalents of the Punfield Formation.
1. Urgonien and Rhodanien of France, Switzerland, &c.
2. Coal-bearing strata of eastern Spain.
VIII. Conclusion.
I. Inrropucrion.
Tux existing scheme of classification of geological formations is in
the main founded on the study of marine strata only. The cir-
cumstance that rocks of freshwater and terrestrial origin occupy
much smaller areas than those of marine character, doubtless in part
accounts for this result, which, however, is to a much greater extent
attributable to the fact that the fossils of the former class of strata
are much less numerous and less strikingly characterized than those
of the latter. With the progress of geological research and its
gradual extension over wider areas, the necessity for successive
enlargements and modifications of our scale of geological periods has
from time to time become manifest. The conclusion, so strongly
insisted upon by Mr. Darwin and Professor Ramsay, that unconformi-
ties between strata indicate the lapse of enormous periods of time, is
being constantly confirmed by the discovery, as fresh districts come
under investigation, or old ones are more accurately studied, of
formations which more or less completely represent these “breaks.”
Not less important in its bearing upon geological theory is the fact
that old and well-known formations, as they are studied at points
more and more remote from the typical district, exhibit new cha-
a2
208 '- PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
racters, and evidence of having been deposited under widely dis-
similar conditions. Thus marine formations are found, not only to
exhibit all the variations consequent on changes from littoral to
deep-sea conditions, but even to pass into or alternate with fresh-
water and terrestrial strata and vice versé. So far have discoveries
of this kind already advanced, that we shall not be going too far in
stating that, in the case of the Mesozoic rocks at least, there is no
great thickness of marine strata with the terrestrial and freshwater
equivalents of which we are altogether unacquainted.
While treating of the peculiarities of the fauna of the period
which lies upon the confines of the Paleozoic and Mesozoic epochs,
Professor Huxley has been led to remark that it will ultimately be
necessary for geologists to establish two parallel but distinct schemes
of classification for strata of different origin, since the breaks
between the marine systems do not correspond with those between
the freshwater and terrestrial. It is nevertheless clear that the
occurrence of terrestrial and freshwater fossils in marine strata
(into which they have been carried down), the existence of certain
organized beings (as some fish) which live indifferently either in
salt or fresh water, the circumstance of the gradual passage between
or alternation of freshwater and marine strata, together with the
facts of their sequence and the nature of their physical relations,
will afford data for correlating, with more or less accuracy, the two
schemes of classification. Regarded from this point of yiew those
strata which are of fluvio-marine origin, and yield at the same time
marine, freshwater, and terrestrial fossils, are of special interest and
value to the geologist. One of the most remarkable formations of
this character I propose to describe in the present paper.
The first example of a great system of strata of freshwater origin
which was clearly recognized by geologists, was the Wealden, the
nature of which was demonstrated by Dr. Mantell in 1822. Its
exact correlation with the marine formations has, up to the present
time, been the subject of frequent controversy ; but recent dis-
coveries in France, England, Spain, and Germany have furnished us
with many of the data requisite for arriving at definite conclusions
upon the subject. In a short sketch read before the British
Association at its last Meeting I attempted to show how perfectly
the inferences with regard to the age of the Wealden-Purbeck to
which we are led by the study of its marine fossils, accord with
those drawn from an examination of its physical relations to the
great marine systems. From both kinds of evidence I have en-
‘deavoured to establish the following propositions :—
1. The deposition of the Wealden strata of the south of England
commenced before the close of the Oolitic period; it continued —
during the whole of the Tithonian, and of the Lower and Middle
Neocomian, and only came to an end at the commencement of the
Upper Neocomian.
2. The deposition of Wealden strata did not extend to the north
of France until the latter portion of the period, and the beds in this
area are greatly diminished in thickness, while they alternate with
1871.] JUDD—PUNFIELD FORMATION. 209
and, in some cases, are subordinate to marine strata of Neocomian
age.
3. The Wealden of northern Germany is the deposit of a different
river from that which formed the Wealden of England and France ;
and the period of its formation, while it commenced at the same
epoch, was of much shorter duration, coming to a conclusion before
the end of the Lower Neocomian.
In this memoir I propose to describe in detail some of the
observations on which these conclusions are founded. Other portions
of the evidence: I am compelled to defer to a future period, the
present state of affairs in France having prevented me from making
certain investigations essential to the completion of the subject.
At the base of the great freshwater system of the Wealden there
is found a series of beds with fluwvio-marie characters, constituting
the well-known “ Purbeck Formation.” At the top of the Wealden
there occurs another series of strata of similar character, less known,
it is true, but not less interesting and important, for which I propose
the name of the “‘ Punfield Formation.”? These two series of beds,
consisting of finely laminated clays, sands, and limestones, while
they present many points of resemblance to one another, are very
distinct both in mineral character and the nature of their fossils
from the purely freshwater and generally brightly coloured beds of
the Wealden proper, as well as from the truly marine beds of the
Oolite and Neocomian. The Purbeck formation is shown by its
stratigraphical relations, and the fossil contents of its marine beds,
to have very close relations with the Oolitic System. The Pun-
field formation is, on similar evidence, clearly referable to a portion
of the Neocomian System. In both the Purbeck and Punfield
formations, we find evidence of the alternation of freshwater,
brackish-water, and marine conditions: while the former affords
proof of the gradual transition of the marine beds of the Upper
Oolites into the freshwater strata of the Wealden, the latter as
clearly indicates the equally gradual return of marine conditions,
which, at the termination of the Wealden period, ushered in the
Upper Neocomian.
These several formations occur in unbroken sequence as follows :—
Upper Neocomian (‘‘ Lower Greensand”’)...... Marine.
Punneld Hormation oF siete Jluvio-marine.
Pep oectehie 25 1562 LK ea eee ULE oki . ehect x Sreshwater.
Parbock Formations (3.45. chs cess vai gisee swede das Sluvio-marine.
MT SOU oasis <canaerm iene he Medina nshide beng? marine.
Il. Breri0GRAPHY OF THE SUBJECT.
Although no special mention of the strata which I am about to
describe is found in the earliest memoir (that of Webster*) on the
Wealden and Purbeck of the Isle of Wight and Dorsetshire, some of
their peculiarities have long been known to local collectors, who
have named the more fossiliferous portions the “ oyster-beds” and
* Letters in Sir Henry Englefield’s ‘ Isle of Wight’ (Trans. Geol. Soc. Ser. 2,
vol. ii. p. 37).
210 "PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
*‘cone-beds.” They were certainly known to Dr. Mantell; and
specimens of their fossils have long been preserved in local museums.
The strata and their remarkable fossils were casually alluded to
by Dr. Fitton in 1836, though their great importance was not at that
time recognized* .
It is to Mr. Godwin-Austen, who in the year 1850 laid before
this Society a collection of the fossils of Punfield, that geologists are
indebted for first calling attention to the great interest attaching to
these remarkable beds. The collection excited at the time much
notice, and Professor Edward Forbes, then engaged in the prepara-
tion of a memoir on the Wealden-Purbeck,.which he unfortunately
did not live to complete, pronounced that the fauna of these beds
(which he recognized as being clearly intercalated in the Wealden
series), while it had an undoubtedly Neocomian aspect, included
a number of new species, and several forms for which a new genus
would have to be created. As we shall see in the sequel, the views
of Professor Forbes have been completely substantiated by the
labours of subsequent observers.
In his Anniversary Address before this Society in 1851, Sir
Charles Lyell made special reference to the remarkable beds at
Punfield, and their bearing upon geological theory +; and in all the
subsequent editions of his ‘ Elements of Geology’ he has alluded to
the subject as one of great importance +t.
In the Rev. John Austin’s little memoir on the Isle of Purbeck,
the beds are briefly described §.
Mr. Godwin-Austen, in his celebrated paper “On the possible
Extension of the Coal-Measures beneath the South-Eastern part of
England” ||, read in May 1855, again referred to the Punfield beds,
and founded some arguments on their existence.
In the same year (1855) appeared the Geological Survey map of
the Isle of Purbeck, the work of Mr. Bristow, upon which a note
points out the existence of marine beds in the upper part of the
Wealden, and gives a list of some of the genera of fossils repre-
sented 4.
Mr. Godwin-Austen presented his collection of Punfield fossils to
the Museum of Practical Geology, where it was supplemented by
the specimens obtained by Professor Edward Forbes and the
collectors of the Survey. Mr. Etheridge, fully recognizing the
great value and importance of these fossils, not only caused them to
be carefully preserved, but, as several of them were of a perishable
nature, had careful drawings of them made by Mr. Bone, the Artist
to the Survey. Being engaged in the study of the fossils of this age,
T some time ago examined this series of fossils, and to my surprise
* Trans. Geol. Soc. Ser. 2, vol. iv. pp. 207 and 228.
+ Quart. Journ. Geol. Soe. vol. vi p. lix.
{ Manual of Geology, 3rd ed. p. 229 (and all subsequent editions).
§ A Guide to the Geology of the Isle of Purbeck &c., by the Rev John H.
Austin, p. 7.
|| Quart. Journ. Geol. Soe. vol. xii. p. 66.
“| Map of the Geological Survey of England and Wales, Sheet 16.
Sia] JUDD-—PUNFIELD FORMATION. 211
and delight recognized in them the fauna of the coal-bearing beds
of Utrillas, in eastern Spain, which has of late years been made
known to us by the works of Vilanova, de Verneuil, Coquand,
Collomb, and de Loriére. I should, perhaps, mention that in
1850 no description of these Spanish beds had, so far as I know,
appeared.
Believing the subject one worthy of careful study, I have devoted
my attention to it for some time past, and embody the results in the
present memoir. In the execution of my task I have been furnished
with much valuable information and advice by Sir C. Lyell, Mr.
Godwin-Austen, Mr. Hulke (who in 1866 examined the beds and
made a collection from them), Mr. Wilcox, of Wareham, and my
colleagues Messrs. Etheridge, Bristow, and Whitaker.
At the late Meeting of the British Association, I gave a general
résumé of the subject ; and in the recently published work, ‘Student’s
Elements of Geology,’ Sir C. Lyell has referred to the beds and
figured one of their most characteristic fossils.
III. Secrions mn THE IstE or PURBECK.
At the northern part of Swanage Bay, and immediately below the
great chalk ridge of Ballard Down, is a little recess in the cliffs
called Punfield Cove (fig 1)*. It is at this point that we find the
most interesting exposure of the strata which I propose to describe.
Regarding this, therefore, as a typical section, and deriving the name
of the formation from the locality, I proceed in the first instance to
give a detailed account of the succession of beds at this point.
1. Punfield Cove. The strata seen here, in descending order (the
whole being nearly vertical), are :—
(1) Upper Chalk with Flints.
(2) Lower Chalk without Flints.
(3) Chalk Marl.
(4) Upper Greensand, with a poor representative of the Gault Clay towards
its lower part, the whole being about 100 feet thick.
(5) A representative of the “ Lower Greensand,” consisting of grey clays
alternating with ferruginous sandy beds, generally destitute of fossils, but
yielding Hxogyra sinuata, Sow., and Panopea neocomiensis, d’Orb. The
formation is not more than 60 feet thick, and thus exhibits a great
diminution from its equivalent in the Isle of Wight. This resultis partly
due to thinning out, and partly to overlap.
Immediately below we find the series of fluvio-marine beds, which
L propose to include in the Punfield formation (see vertical sec-
tions, fig. 2) :—
A. Dark blue, finely laminated shales, in part cypridiferous, with
thin bands of limestone made up of Cyrena, Ostrea, &c., and fibrous
carbonate of lime (“ beef” or “ bacon ” ), like that of the Purbecks.
According to Mr. Godwin-Austen these beds are only a few feet
thick. At the present time they are completely hidden by the
débris from the beds above, and I have never yet had an opportunity
of seeing them im srtu. They appear, however, to resemble in
* See also Sir Henry Englefield’s ‘Isle of Wight’ (1816), plate 29, no. 1.
212
Fig. 1.—Section eaposed in Punfield Cove..
Oyster-
beds.
Variegated Beds of the Wealden.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
SLM «4444, Lo,
y
CES,
every respect the beds which are
so well developed on the same
horizon in the Isle of Wight; and
the following fossils are recorded
from them by Dr. Fitton.
Cypridea tuberculata, Sow., sp.
valdensis, Sow., sp.
Melanopsis attenuata, Sovw., sp.
tricarinata, Sow., sp.
Cyrena media, Sow., sp.
membranacea, Sow., sp.
Cardium ?, sp.
Ostrea, sp.
These beds have been re-
garded by some geologists as the
greatly attenuated representa-
tive of the Weald Clay.
B. A series of more or less fer-
ruginous sands passing” down-
wards into interlaminated sands
and clays with some seams of
lignite, and containing in its
middle portion several bands of
ferrugineo-calcareous rock, with
oysters and other marine shells.
This series of beds, which is
about 153 feet thick, greatly re-
sembles, in many of its cha-
racters, portions of the Bagshot
series and of the Northampton
Sand. It was in these beds that
Professor John Phillips obtained
the fossil fruit which he de-
scribed before this Society in
1858 *.
The oyster-beds cannot be
conveniently examined im situ,
as they are exposed in a very
inaccessible part of the cliff ; but
facilities for collecting their
fossils are afforded by the great
slipped masses which le lower
down and nearer the shore.
They consist of sandy iron-
stones, in places becoming eal-
careous from the abundance
of oysters and other shells, and
uppear to be very irregular in
* Quart. Journ. Geol. Soc. vol. xy.
p. 46.
1871.]
Fig. 2. Section of the Punfield Formation,
N. side of Swanage Bay.
Scale Lin. to 20 ft.
“Lower Greensand” (Upper Neo-
comian).
aca
" Grey cypridiferous shales, with
bands of limestone, (Cyrena, Oys-
ters, &c.), “beef.”
Cream-coloured and yellow sands
passing into thick-, irregularly
bedded ironstones.
Ash-coloured and yellow sands, with
seams and bands of ironstone
(Oyster-beds). :
Grey and ash-coloured sandy clay,
with bands of ironstone.
Bright yellow sands passing into
ironstone.
Ore toeran
_ Whitish and carbonaceous clays.
a
—Sear Ash-coloured and. yellow sands,
= with thin irregular wavy seams
of light and dark blue clay, and
bands and patches of imperfect
brown ironstone.
Ash-coloured and yellow sands,
with thin irregular wavy seams of
light and dark-blue clay, and
bands and patches of lignite and
imperfect brown ironstone.
Marine band.
Variegated beds of the Wealden.
JUDD—PUNFIELD
BARNES SERIES.
FORMATION. 213
Fig. 3. Section of the Punfield Formation
in the Isle of Wight.
Seale 1 in. to 20 ft.
“ Perna-beds”’ (Upper Neocomian).
Green clays.
Dark grey finely-laminated shales
in places abounding with Oypris.
Bands of limestone with “beef” and
“cinder,” Oyrena and Ostrea abun-
4 _ dant.
Dark grey shales with a few bands
of sandstone, Cypris and Paludina.
Limestones with Ostrea, Modiola,
Cardium, and other marine shells.
Dark-coloured shales and mars,
cypridiferous in places.
“ Bone-band,” shales, and thin
bands of limestone (Cyrena).
COWLEAZE SERIES.
Grey paper-shales with sandy and
limestone bands.
Some bands of lignite and nodules
of pyrites.
Beds of yellow sand, very irregular
and inconstant.
Dark grey and black shales, with
bands of shell limestone.
Oyster-beds, sandy and septariiform
layers.
Irregular and inconstant beds of
yellow sand.
Dark grey shales, with bands of
limestone, &c.
Bed of hard ferruginous sandstone
with pyrites, Ostrea, Qyrena, &c.
\
False-bedded yellow sands and
sand-rock, very ferruginous in
places.
Alternations of finely laminated
clay and sand, with some seams
and patches of lignite.
{—
Variegated beds of the Wealden.
214 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 8,
their mode of occurrence. Sometimes we find a thick ferruginous
rock, the bedding-planes of which are covered with thin layers of
oysters ; at other times a hard blue-hearted calcareous rock, emitting
a fetid odour under the hammer, and almost wholly made up of
oysters and other marine shells. The oyster-beds usually contain a
large quantity of carbonaceous matter, and in places, indeed, pass
into what might be called impure lignite. The thickest of them
measures about four feet, and it contains several interstratified bands
of clay, which, like the similar beds below, contain many small
oysters scattered through it.
The fossils of these oyster-beds appear to be for the most part
marme. By far the most abundant are two species of oysters, one
plain, the other plicated. A careful comparison of a large series of
these convinces me that they are dwarfed forms of Hxoyyra sinuata
Sow., and #. Boussingaultwi, D’Orb. Almost all the shells found
in these beds appear to be stunted in their growth, probably from
haying lived under unfavourable conditions. No specimens of
Ammonites have been obtained from these beds, and only one small
and doubtful example of a Vicarya. The following are the fossils
hitherto obtained from the oyster-beds of Punfield.
Exogyra sinuata, Sow.(very abundant) , Corbula striatula, Sow. (abundant).
Boussingaultii, D’ Orb.(veryabun- | Anomia leevigata, Sow. (abundant).
dant). Modiola giffreana, Pict. et Roux
Pecten, sp. (very small). (rare).
Cardium subhillanum, Leym. (rather
rare).
Several small univalves.
Much carbonized wood.
In the same part of the series as the oyster-beds there occurs a
bed of Sandstone containing Cyprides and casts of Cyrena.
C. “The Marine Band of Punfield.” This bed, though only
21 inches thick, is of the greatest interest, presenting us as it does
with a very considerable marine fauna, and thus furnishing the
means of correlating this portion of the Wealden with the series
of marine formations. It forms a well-marked feature in the cliff
at Punfield Cove, dipping due N. at an angle of 65°. In its general
characters it is very similar to the oyster-beds above. The oysters
in this bed, which are of the same species as those in the oyster-beds
(Exogyra sinuata and EH. Boussingaultz), attain however to a
larger size, and approach more nearly to their normal forms than in
the latter beds. The specimens of Corbula striatula and Cardium
subhillanum likewise attain to larger dimensions. But besides the
shells which occur in the oyster-beds, we find in this band many which
are much more decidedly marine, including Ammonites Deshayesi,
several forms belonging to the new genus Vicarya, and species
of Trochus, Natica, Actwon, Actwonella, Orthostoma, Pholadomya,
&e.
The upper part of the marine band consists of a hard laminated
micaceous sandstone, more or less calcareous, containing much
iS fale JUDD—PUNFIELD FORMATION. ’ 215
carbonaceous matter and sometimes becoming perfectly black and
resembling an impure lignite. This portion of the bed contains
but few shells, and passes by insensible gradations into the inter-
laminated sands and clays above.
The middle portion of the marine band is almost wholly made up
of oyster-shells, with a few dwarfed specimens of Corbula, Cyrena (?),
and Cardium. Like the upper portion it contains very much car-
bonaceous matter. I have not obtained from this portion any
specimens of Ammonites or Vicarya.
The lowest portion of the marine band to the thickness of 6 or 8
inches is a hard, more or less ferruginous, very shelly limestone of
a blue colour, weathering brown at the joints, and containing
numerous pebbles or concretions composed of argillaceous limestone.
This bed of hard limestone is traversed by some irregular seams of
hard blue clay or shale ; it contains comparatively little carbonaceous
matter, but yields Ammonites, Vicarya, and other marine shells.
The oysters in this portion of the marine band are sometimes large
and approach very closely to their typical forms*.
Almost immediately underlying the marine band are the varie-
gated Wealden Clays and Sands, which in Swanage Bay attain
probably to a thickness of nearly 2000 feet, and yield, so far as
I know, only the remains of freshwater and terrestrial forms of
life.
The following fossils have been obtained from the marine bands
of Punfieldt.
Teeth of Lamna, sp. Orthostoma Verneuili, Valanova, sp.
—— Pycnodus, sp. Exogyra Boussingaulti, D’ Ord.
Ammonites Deshayesii, Leym. sinuata, Sow. (dwarfed).
Vicarya pizcuetana, Vilanova, sp. Anomia levigata, Sow.
Lujani, De Verneuil et Collomb. Plicatula asperrima, D’ Orb.
Pradoi, De Vernewil et DeLoriére. | Perna Rauliniana, Pictet et Roux.
Cerithium Vilanovee, De Vernewil et De | Modiola giffreana, Pictet et Rows.
Lorieére. Arca cymodoce, H. Coguand (young).
Pailleti, De Verneuil et De Loriére. | Arca, sp.
Turritella Tournali, H. Coguand. Cardium subhillanum, Leym.
Pleurotoma Utrillasi, De Verneuil et impressum, Desh.
De Loriére. Astarte, sp.
Fusus (?) neocomiensis, D’ Orb. Isocardia nasuta, H. Coguand.
Actzon Esquere, De Vernewil et De , Sp.
Loriére. Leda scaphoides, Pictet et Campiche.
pradoana, De Vernewil et De | Tellina? gibba, H. Coquand.
Loriére. Corbula striatula, Sow.
Acteeonella oliviformis, H. Coquand. Pholadomya semicostata, Aq.
Trochus Esquerz, De Verneuil et De | Pholadidea (borings).
Lorieére. Serpula.
Natica levigata, Desh., sp. Numeroussmall univalves and bivalves,
pradoana, Vilanova. fragmentary and undeterminable.
Neritopsis minima, De Verneuil et De | Much wood and carbonaceous matter.
Loriére. i
* Mr. Etheridge is engaged in the preparation of descriptions of those
fossils of the Punfield formation which are new to this country.
+ Since the reading of this paper, Mr. C. J. A. Meyer, F.G.S., informs me
Fig. 4.—Section exposed in Worborrow Bay.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
Purbeck.
Variegated Beds of the Wealden.
Marine
Band
Upper
Neocomian.
soe ek
Gault.
|
a. !
Alc)
Apis
Upper
Greensand,
le.
\\ = fies
ay,
2. Worborrow Bay. I have not
been able to find any inland sections
in the Isle of Purbeck which throw
light on the Punfield formation. But
at the western end of the peninsula,
in the cliffs of Worborrow Bay, 11
miles distant from Swanage Bay, we
find another exposure of these beds.
At this place the Chalk, Chalk-marl,
Upper Greensand, and Gault present
the same characters as in Punfield
Cove, and, as there, are inclined at a
high angle (fig. 3) *.
The Upper Neocomian (‘ Lower
Greensand’’) is represented by about
_ 40 feet of clays, sands, and ironstones.
From these beds I obtained a fine
specimen of the highly characteristic
Panopea neocomensis.
The Punfield formation is here
about 65 feet thick. No trace of
the blue clays with limestone bands
oyster-beds and “‘ beef” is found in its
upper part; but its whole thickness is
composed of interlaminated clays and
sands, with lignite and bands of iron-
stone containing a few apparently
marine shells. At the base is a very
distinctly marked bed of ironstone of
a dark reddish-brown colour, contain-
ing casts of shells, which were re-
cognized by Prof. Edward Forbes as
marine. The presence of this bed is
recorded in a note on the Map of the
Geological Survey. The general suc-
cession of the Punfield-beds at Wor-
| borrow Bay is as follows :—
| that he has examined the Punfield section
and found a single specimen of the genus
Arca, the species being indeterminable,
some feet below the Marine Band. ‘This
|| discovery is interesting as a fresh proof of
the gradual nature of the change from
freshwater to marine conditions.
* See also Sir Henry Englefield’s ‘Isle
| of Wight,’ Plate 37, No. 1.
Chalk.
1871. } JUDD—PUNFIELD FORMATION. 217
a. Beds of light-coloured sometimes pinkish sand, in places
interlaminated with bands of clay. They contain much
carbonaceous matter, seams of lignite and nodules of
[OURO a peeeddcadl aan ebe aaso one seacenstn ose deypoberUbeneasaeneened about 30 ft.
6. Beds of grey and whitish laminated clay (with much
lignite in places) and bands of nodular ironstone. These
ironstones contain casts of shells, very imperfectly pre-
served, including Ostrea, Cardiwm, Corbula, and Ceri-
thium. I regard these as the equivalent of the ‘‘ oyster-
[oeGlS) Ort TENANCE? coopenccacadasad aansooasocsddoosbeos9p00anR0R0cq 30 to 40 ft,
e. Thin well-marked band of ironstone, very hard and dark-
coloured, only a few inches thick. This bed is in
places crowded with vegetable markings, and contains
casts of marine shells. This bed rests directly upon the
variegated beds of the Wealden, and seems to represent
the “marine band of Punfield.”
3. Mewps Bay. At this place, which is 13 mile W. of Wor-
borrow Bay, the very diminished representative. of the Upper
Neocomian (“ Lower Greensand ”) is faulted against the variegated
beds of the Wealden. The same is the case in Bacon Hole a little
farther west.
4. Lulworth Cove. This section is about one mile west of the
former. On the eastern side we find lying directly upon the varie-
gated beds grey clays with ferruginous bands containing much
wood and vegetable matter, and also a few casts of shells, none of
which are determinable. There appears to be here no trace of the
Upper Neocomian (Lower Greensand), which is probably either
quite overlapped by the overlying Cretaceous beds, or has altogether
thinned out.
TY. Srcrrons 1n THE Isuz oF WiGHT.
The nearest Isle-of-Wight section of the Wealden strata, that of
Compton Bay, is situated thirty miles due east of Punfield Cove.
As, however, the clearest exhibition of the representatives of the
Punfield formation is that in Brixton Bay, a little to the west of
Atherfield Point, I propose in the first place to describe this in
some detail, and then to point out in what respects the sections of
Compton Bay and Sandown Bay differ from it.
Considerable diversity of opinion has existed among geologists with
regard to the correlation of the Wealden beds of the Isle-of-Wight
with those of the Weald-area of Kent, Surrey and Sussex.
While Dr. Fitton * regards the upper grey shales and limestones as
representative of the Weald Clay, and the sands and variegated
beds below, as equivalent to the Hastings Sand, Mr. Bristow tf
considers the whole of the Isle-of-Wight series referable to the
former subdivision, and believes that the latter is not represented in
the island. The manner in which the Wealden beds thin out
rapidly, or change their mineral character laterally within short
distances, will always render any attempt at correlating their sub-
_ * Trans. Geol. Soc. Ser. 2, vol. iv. p. 184, et seq.
+ Memoirs of the Geological Survey, Geology of the Isle of Wight (1862), p. 8.
218 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
divisions over a considerable area a very doubtful and difficult task.
In the present paper I propose to include in the Punfield formation
those beds at the top of the series which present the same mineralo-
gical characters as the typical beds of Punfield Cove, and which,
like them, show signs of flwvio-marine origin in their intercalated
bands of marine shells. The great mass of variegated strata con-
taining only freshwater and terrestrial fossils I regard as the Wealden
proper.
1. Brixton Bay. The Punfield strata are seen here between
Atherfield Point and Barnes High. They are well illustrated in the
detailed section of Professor E. Forbes and Mr. H. W. Bristow *.
Their junction with the overlying “‘ Perna-beds of the Upper Neo-
comian” is fully described by Dr. Fitton, who had a favourable
opportunity for observing it in 1847+; this junction is now con-
cealed. The Punfield strata of the Isle of Wight, which attain a
thickness of 230 feet, fall naturally into two groups, which, for the
sake of convenience in description, I have distinguished by local
names (see vertical section, fig. 3).
A. The Cowleaze Series, consisting of dark grey, blue, or green
cypridiferous shales and clays, with indurated sandy ferruginous
and argillaceous bands, and thin beds of limestone crowded with
shells, Paludina, Cyrena, Cerithium, Melanopsis, Unio, &e. << Beef,”
or fibrous carbonate of lime, occurs abundantly in these limestones,
which not unfrequently contain marine shells, and are sometimes quite
made up of small oysters, when they exactly resemble the well-known
‘“‘Cinder-bed” of the Purbeck series. It is evident that the
Cowleaze series was deposited under conditions very similar to those
which prevailed during the formation of the Purbecks. While,
however, in the latter the clays are subordinate. to the limestones,
in the former the limestones are much less developed than the clays.
The thickness of the Cowleaze series is about 180 feet; and the best
exposure of it is in Cowleaze Chine, where nearly 100 feet of its
lower portion is exhibited in a clear section. The Cowleaze beds
contain in places plant-remains ; and in some of the bands teeth and
scales of fish are very abundant. Among the marine shells occur
Exogyra sinuata and E. Boussingaultn, both much dwarfed, also
Modiola (two species), Cardiwm, and Cerithium. Iam not aware
- that any Ammonites have been found in these beds in Brixton
Bay, though an undoubted specimen was obtained from them at
Red Cliffin Sandown Bay. The limestone bands of the Cowleaze
series are used locally, like those of the Purbecks, for rough
aving.
x B. The Barnes Series. These beds rise from the shore at Cowleaze
Chine, ard crop out at the surface at Barnes High. Owing to the
superior hardness of their upper beds they make a very marked
feature and can easily be traced inland through the island. While
* Memoirs of the Geological Survey, Geology of the Isle of Wight (1862),
plate 2. fig. 2.
+ Proc. Geol. Soc. vol. iv. p. 198 ; Quart. Journ. Geol. Soc. vol. ui. p. 293.
1871.] JUDD—PUNFIELD FORMATION. 219
in the Cowleaze series the argillaceous element preponderates, the
Barnes beds are in great part composed of sand or sandstone, with
subordinate bands of clay. The following is the succession of beds
in Brixton Bay.
(a) Very hard greenish-white sandstone, with many nodules
and veins of pyrites; shells numerous in its upper part _—1 to 2 feet.
(6) Less hard coarse greenish sandstone forming a ledge
above the beds below ...............ceecececseteeceeeserseeees 4 to 6 feet.
(c) Yellow false-bedded sand slightly ferruginous in its
upper part, carbonaceous im places .....+...seeeeeeeeee eee 25 to 30 feet.
(d) The lower portion of the last graduates downwards into
interlaminated sands and grey micaceous sandy clays... 15 feet.
Ke eWellow, and wihite) SartGs) eercscssecacsnusospncuarstesciedsee nase 3 feet
These beds rest on the ordinary variegated strata of the Wealden,
which are exposed to a thickness of from 300 to 400 feet; but their
base is not visible in the Isle of Wight.
The sandy beds of the Barnes series usually contain but few
shells. The top band of sandstone exhibits Cyrena and Unio in
abundance, but, owing to the hardness of the matrix and the decom-
posed condition of the shells, the fossils are very difficult of extrac-
tion. In places the beds contain much carbonaceous matter, with
seams of lignite and masses of wood converted into jet or pyrites.
One band has yielded marine shells, including oysters, Cardium,
casts of Trigonia, and several univalves. The beds of the Barnes
series have furnished to local collectors a rich harvest of reptilian
bones *.
It seems not improbable that the thin beds (A) at the top of the
section in Punfield Cove represent, in a very attenuated condition,
the Cowleaze series of the Isle of Wight, while the beds below
(B and C), are an expanded form of the Barnes series.
2. Compton Bay. The Punfield strata are here highly inclined,
and are broken up by several faults, They are well illustrated in
the section of Professor Forbes and Mr. Bristow +. The Cowleaze
series, with its Cyrena- and Paludina-limestones and “beef” and
*‘ cinder ” beds, is well exposed. Besides the two species of oyster,
the marine bands yield Panopea plicata, Sow. (small), Serpule, and
numerous fish-scales. The beds, being repeated on the shore by a
fault, afford great facilities for the collection of their fossils. The
Barnes series presents its usual sandy characters, and is about
50 feet thick. It contains several beds with plants and insects ; but
I did not here observe any marine bands in it.
3. Sandown Bay. On the south-west side of this bay the Punfield
beds are quite concealed, forming low ground covered by vegeta-
tion ; but on the north-east side of the bay, below the Red Cliff, the
strata in question are well exposed. By a recent slip in the cliff
the junction of the Upper Neocomian and Wealden is well exposed
(1870), and yields the following section.
* Quart. Journ. Geol. Soc. vol. xxvi.
+ Memoirs of the Geological Survey, P eeslogy of the Isle of Wight, plate 2.
fig. 1.
220 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
(a) Atherfield Clay. Grey clay with usual characters... 4 to 5 feet, seen.
(6) Perna-beds with usual characters, but more weathered
than at Atherfield, and ofa brown instead of a green
colour ; consisting of the following divisions :—
a. Hard brown sandstone (fossils very abundant).
Perna Mulleti, Desh.
Hxogyra sinuata, Sow.
Gervillia anceps, Desh.
Panopza plicata, Sow.
Modiola.
Pecten, sp.
Trigonia aliformis, Park.
Thickness rather irregular but ............:..::ccsseeeee about 2 feet.
(This bed passes gradually into)
B. Greenish-grey sandy clay with many fossils ......... nearly 4 feet.
y. Bed similar to a, with Ancyloceras and other shells 1 foot.
(passing in its lower part into greenish-grey sandy
clay, and so into)
(c) Blue paper-shales of the Wealden .................0.00+- 9 inches.
(d) light-coloured and pyvitic..........s0.e0+-++2-0ec00e 1 foot.
(e) Dark-coloured paper shales (with Cypridea valdensis)
and several layers of nodular ironstone ............... 4 feet?
(A): SBeektPal moby See Re Mee EMA i tae
Limestone crowded with Cyrena and a few oysters,
6 i 9 inches.
INCHES!) smalteswoeancys vom tnane « assanegecins acetone seane
‘Beet Zito inches: Ay sat ovens sakes sentausiane eee
(g) Finely laminated pyritic clay..,................00:s00000 9 inches.
(2) Ferruginous band almost entirely made up of shells
(oysters and small univales) ...............02:0eeeeeeeeeee 3 inches.
(%) Other beds of dark blue laminated shales, with oc- between
casional beds of limestone, imperfectly exposed... { 30 to 40 feet seen.
The total thickness of the Cowleaze series cannot be exactly
measured in Sandown Bay. In the marine bands I found Hxogyra
sinuata, Sow., EH. Boussingaultii, D’Orb., Corbula striatula, Sow.,
Cardium subhillanum, Leym., with vertebre and teeth of fish
(Lepidotus, &c.), and plant-remains. In one of the ‘‘ Cinder ” beds
at this place Dr. Fitton found an imperfect but undoubted specimen
of an Ammonites *, and I have myself obtained what appears to be a
fragment of Ammonites Deshayesii, Leym. The yellow sands of the
Barnes series are seen in Sandown Bay, and where they come to
the surface form a well-marked escarpment, that on which Yaver-
land Fort is built. Here, however, the beds are not favourably
situated for examination.
VY. Secrions IN THE WEALD oF Sussex, SURREY, anD Kent,
The Wealden strata of this area, presenting few exposures in
sea-cliffs, are not so well known as those of the Isle of Wight and
Dorsetshire ; but there are not wanting indications that, like these
latter, they graduate upwards through fluvio-marine beds into the
Upper Neocomian, which everywhere conformably overlies them.
1. Leith Hill. In the Museum of this Society there is a series of
fossils from Leith Hill, near Guildford, accompanied by a section in
which the marine beds at the base of the “‘ Lower Greensand ” are
* Trans. Geol. Soc. 2nd Ser. vol. iv. p. 190.
1871.] JUDD—PUNFIELD FORMATION. 221
represented as alternating with freshwater beds full of Paludine
and other Wealden fossils. This series of fossils was presented to
the Society by D. D. Heath, Esq.
2. Hythe. At this place Mr. Mackeson discovered, about 30 feet
below the top of the Weald Clay, beds of limestone crowded with
oysters *; and similar beds in a like position have been noticed by
Mr. Simms and other observers }.
VI. Retations or THE PuNFIELD ForMATION To THE WEALDEN,
Neocom1an, AND CRETACEOUS OF THE SoutH oF ENGLAND.
1. Unconformity between the Cretaceous and Neocomian.— We
are indebted to the late Captain Ibbetson for first clearly demon-
strating the existence of an unconformity between the Cretaceous
proper and the Neocomian in the South of England+. By a series
of careful trigonometrical observations he showed that, while the
Chalk, Upper Greensand, and Gault beds in the south of the Isle of
Wight are nearly horizontal, the Neocomian and Wealden dip to the
east at an angle of about 2°. The effects of this unconformity are
most striking, the beds of Cretaceous age overlapping in succession
all the beds of the Oolite and Lias, and resting, in Devonshire, on the
New Red. The same effect of overlap through unconformity was,
at an earlier date, demonstrated in Yorkshire by the labours of
Smith and Phillips; and I have shown that the same phenomenon is
exhibited in Lincolnshire. The work of the Geological Survey has
proved that a similar overlap of the Cretaceous occurs all round the
Weald, and throughout the Midland district, so far as the survey has
been carried. Every geologist is familiar with the fact that the
same phenomenon of unconformity is exhibited between the Creta-
ceous and Neocomian strata of France and Switzerland. Professor
Ramsay has shown from Mr. Etheridge’s Tables that this unconfor-
mity is accompanied by a very great change between the faunas of
the two series of strata §.
2. Variation in character of the Cretaceous in proceeding from
East to West.—That the Upper Cretaceous does not terminate down-
wards with the “ junction-bed ” at the base of the Gault Clay has
been noticed by several geologists, who have shown that the sands
immediately below that clay contain characteristic species of Gault
Ammonites. That the same is true of the corresponding beds on the
east side of the Paris basin, is shown by the able researches of
M. Cornuel, in the department of the Haute Marne ||. As the base
of the true Cretaceous and the top of the Neocomian are thus
alike composed of sands which are usually very unfossiliferous, it
often becomes a question of great difficulty where the boundary
* Mem. of Geol. Survey, Geology of country between Folkestone and Rye,
by F. Drew (1864), p. 6.
t Proc. Geol. Soc. vol. iv. p. 208.
{ Quart. Journ. Geol. Soe. vol. iii. p. 315.
§ Quart. Journ. Geol. Soc. vol. xx. p. 58. }
| Bull. de la Soc. Géol. de France, 2° sér. tome. xvii. p. 743; Wiltshire,
Quart. Journ. Geol. Soc. vol. xxiv. p. 483, in Discussion.
VOL. XXVII.—PART I. R
222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Feb. 8,
between them should be drawn. Mr. Godwin-Austen has remarked
on the close connexion between the Upper Greensand and the
Gault, and is inclined to consider their differences due rather to
the conditions than to the time of deposition. Probably we should
be near the truth in representing the Upper Greensand and Gault
as one formation, with arenaceous characters prevailing in its lower
part, and inconstant and irregularly developed beds of clay in its
midst. In Kent these beds of clay are thick, well defined, and
sharply separated from the sands above and below; but in the
Isle of Wight they are much less strikingly characterized ; and as we
proceed eastward they thin out and finally disappear in the neigh-
bourhood of White Nore, in Dorsetshire. Thus in the Blackdown
beds of Devonshire we have the representatives of the sands above
the Gault Clay and those below it brought together, a fact which
may account for the anomalous character of the fauna of those beds.
It is not, however, improbable that these western portions of the
Cretaceous series, like certain similar deposits in the north-west of
France, may be of somewhat earlier date than those of the east of
England, though continuous with them, and may thus represent the
latter part of that great period which must have elapsed between
the Neocomian and the Cretaceous. It must be remembered, how-
ever, that the Ammonites of the Blackdown beds are nearly all well-
known Gault species. My friend Dr. Lycett informs me, too, that
the supposed correspondence betwen the Trigonie of the Blackdown
beds and those of the Neocomian breaks down on a careful and
critical examination of the specimens. It is not improbable that
some other of the supposed anomalies of the fauna of the Black-
down beds would also disappear on a more careful examination of
the fossils.
3. Thinning-out westward of the Neocomian and Wealden.—
Nothing can be more striking than the great difference between the
thickness of the beds which lie between the Chalk and the Portland in
Swanage Bay, and in the section of Man-of-War’s Cove and Durdle
Cove. This effect is, as we have already seen, partly due to overlap ;
but in a much greater degree it is owing to the tendency which all
these beds have to thin away towards the west. From the very
detailed sections published by the Geological Survey * (the work of
Messrs. Bristow, Whitaker, and the Rev. O. Fisher), and from my
measurements, the accompanying Table has been constructed, which
shows in what a very marked manner this attenuation of all the
beds towards the west takes place. Of this general tendency the
Punfield formation partakes. Mr. Whitaker has recently shown
that the lower beds of the Chalk exhibit a similar thinning-out
towards the west.
4, Relation of the Purbeck to the Wealden.—At the only points
where the junction of the Purbeck and Wealden is clearly seen,
namely in Worborrow Bay and Mewps Bay, the marls with
Paludine, which form the top of the Purbeck, are seen to pass, by
* Geological Survey in England and Wales, Horizontal Sections, Sheet 56,
and Vertical Sections, Sheet 22.
ta.
[To face p. 222
a
t side of
ae Cove.
feet
“LOWER GREEN).
PUNFIELD FOR} ont
WEHALDEN ...... 462
Paludina-Clays 39 ™
Upper Cypris-Clag
Unio-Beds ...... 6 4
Upper Broken Shy 9
Total Upper 4 6
Chief Beef Beds 2,
Corbula-Beds ae
Scallop-Beds rc
Intermarine ...... 7 8
Cinder Bed ...... 4 0
Cherty Freshwate, 9
Marly Freshwater
Total Middleg 4
Marly Freshwater, 3
(Upper Insect-Be¢
Soft Cockle-Beds
poeccce
7
Hard Cockle-Bed 7
(Lower Insect-Beq
Cypris-Freestones, 6
Broken Bands ...5
Soft Cap ........04 1 6
Hard Cap.........| 4 6
Total Lower, 3
PURBECK FORM; 1)
WEALDEN-PURBE 46
Man-of-War :
i Gee * Ridgeway.
feet feet
absent absent
absent absent
172 ?
tt ap
Soe 5. HO
suede 26 4
BES QO Ff
Braise to. 6
see 52 3
Bee A dk
pooaas 18 6
Le Sabi a &
conus Gy 89
so008 & ©
iat 6 8
ei 47 7
seen Aly)
Wasa 5 ©)
es Ap
ADDOGC SLL
BRAS B®
ga0ni6 A) Gi
Lanes 3
Beene \ Be
Savteee 94 0
100? 193 10
(2170) ta an Fa cat
a
Table illustrating the thinning-out Westward of the Neocomian and Wealden Strata.
“LOWER GREENSAND”
PUNFIELD FORMATION.............06+4
WEALDEN
Pee eee errr eee
WEALDEN-PURBECK
Paludina-Clays ...ccccsecseseceserecreceerees
Upper Cypris-Clays and Shales............
Unio-Beds
Total Upper Purbeck ...............
Chief Beef Beds ...
Corbula-Beds
Scallop-Beds
IPONIN ENING eseccctvcecescersr<astsecsneter ess:
Cinder Bed .........
Cherty Freshwater
Marly Freshwater
Seen meee nee e en eeenneeeeeenseeaes
eee e eee e nee e reese eee netnsnteenes
See e eee eweetesereteereceee
Total Middle Purbeck ............
Marly Freshwater .......::sccssesescsseeeees
(Upper Insect-Beds) ....:+....0seeceeeeeeees
Soft Cockle-Beds ....c....s:scccceereeees
Hard Cockle-Beds ..,....scsccssscssscenyeees
(Lower Insect-Beds) ............eeseeeeeeess
Cypris-Freestones ..sssececeessseceees cube
Broken Bands
HOO eee e eee n sent e eee seneeeeneeeeeetees
wee neeeeeeeeeee
PURBECK FORMATION
Aen eee eetee eee eeenes
[To face p. 222
Worb Hast side of | Man-of-W: a
Atherfield. |Compton oe Bay. gic! Mewps Bay- | Tulworth Goset P OnE. a Ridgeway.
feet feet feet feet feet feet feet feet
802 500? 452 36 absent absent absent absent
230 200 160 65 re absent absent absent
unknown unknown 1800 725 660 462 172 ?
ft. in. ft. in ft. in. ff. in ft. in.
eee (alee ee 18? 13? mo 8? See 5. ro
Sue | eed aban 47 10 36 «9 28 11 1p 7 stinae 26) #
feat. |) = padoog wy) 16 ° ye caterer 9 = %
niboros © Malfe Se= doesn 5 Coe) 7 <0 iG} By =9) res Moje 1
PEE Mies \Sedonds 80 7 73 3 52 2 34 6 SA 52 3s
oper dR. pGeK00 30 +O 13 10 6 6 Bo nae Aas
Spocen, Sia esdeoss Aer) 39 9 22 7 Fey nity Becets 18 6
odnta ee) ENS sencbd 4 6 2) 9 ZA: I 10 naan coxens
Seccen = fe onpenen 46 o ° Sane, We a5 pantie 7) a8
aoc. |) want 8 6 5 6 4 0 4 © teens Re
pone Potions 28 «66 18 3 aay! Feo) S90 Ge A
nepoe® ble cen Bd i) 350027 00 ot pee nenged (he oa
aocads. | le atbacrs 155 8 89 1 49 7 43 1 deseoe ise
medio | lee 8 undoon a) ite) Ties 8 0 res. 44 eben Aaa
Pere (rire (poceerrrcmeen (icrcc: | A Coosccccss | he ochmenrce, © cotanc 520
recto ous -pabont 82 62) 97 58 Cl EG | cord 27
exoog | = a ee—cneece 10) By (8) 24 4 ra) 7, coveee 8 4
Sedan octfe 2 oldssess — 1B Gdewesss as |P™ — ieeeatam aeumn| Ole lies Sces ct stianns | aes cone | Cece Bae
onion © fh ecuoeD 36 3 26 «5 Ig 10 21 10 sudpe 26 67
Some, & cake Lapione 5) 50 57 a} 15) 40 Io oO soci 9
SSacedc. ten|| es = ceetec WieiO 5 6 | ee) a 6 Serre } roe
Sone ey nn | Poe ass sen Tr 3 6 3 Sy fey | <6 wae
Scat lice eases 169 10 151 6 I5E 2 106 3 sevens 94 0
ea elie sone 406 1 3138 10 252 10 183 10 100? 193 10
ee rhe sete 2366 1104" 913 646 272 sees
degArnes |
far
FA we ee
ee 1
pat a
wie
’
os
tee .
A
> i re
Thee Se
Te ae
et Z
oe tyes Oe ,
*
Als
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SEN) eee
iM Fics
pes
“ '
PO eee
ante
Wut
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+6 ed
pe :
ri
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: F
Pte eae
es
A
r
eh Shik Mediates
red Si 5 >
Rien rte Peay | Ni Saea's ae
a
i ee
Ape oct page Gos ca btn
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Vey bem sath Sheet ry ies’
fy
bs
f
He DER Eve eA iees
hats HTP ae Dew ee
¥ Piytele lt ew ele w
Clad eh as?
1871.] JUDD—PUNFIELD FORMATION. 223
insensible gradations, into the variegated clays and sands of the
Wealden. The same is described as taking place in the section
(now concealed) of the Ridgway Cutting by the Rev. Osmond Fisher *.
It is true that Professor Forbes pointed out that, if we compare the
shells of the Purbeck with those of the Wealden, we shall find very
few species that; are common to both. When, however, we consider
the fact that the great majority of the Mollusca and Entomostraca
which are regarded as typical of the Wealden have been obtained
only from the higher portions of the series, the fact will be seen to
have but little significance. As is well known, the Purbeck (like
the Punfield series) includes certain beds which are of a decidedly
marine character and contain shells undistinguishable from common
Oolitic species, with an Echinoderm (Hemicidaris purbeckensis,
Forbes) which, though not occurring in the marine series of this
country, is found in the Upper Oolite of the Jura. Not only is the
passage of the Portland into the Purbecks a gradual one in the
typical country of these formations, but, as Mr. Godwin-Austen
has shown, we find at Swindon Purbeck beds actually alternating
with the Portland rocks ft.
As no break has ever been shown to exist in the succession of
Wealden beds in the south of England, we are compelled to conclude
that they represent the whole of the vast interval between the
Upper Oolite and the Upper Neocomian.
VIL. Forrren Equrvatents oF THE PuNnFIELD FoRMATION.
1. “ Urgonien” and “ Rhodanien” of France, Switzerland, &c.
—That the strata known as “ Lower Greensand” in England re-
present the “‘ Aptien”’ or upper division of the great Neocomian
system of Continental authors has long been recognized by geolo-
gists. The very careful study of the fossils of the different portions
of the Neocomian by Pictet, Renevier, and other paleontologists
has established this correlation in the most satisfactory manner.
The beds of white limestone, crowded with shells of the order Rudistes
(Chama, Anomia, &c.), and with corals, which constitute the ‘“ Ur-
gonien” of D’Orbigny, and are so widely distributed in Southern
Kurope, have everywhere been recognized, both on stratigraphical
and paleontological grounds, as constituting the middle portion of
the Neocomian system. In the year 1854 M. Renevier, of Lausanne,
who has devoted so large a portion of his studies, with the most valu-
able results, to the beds of this age, showed that between the “ Ap-
tien”’ and ‘“‘ Urgonien” another series of beds with a distinctive fauna
was recognizable, for which he proposed the name of “ Rhodanien”+.
To this subformation M. Renevier, after a careful personal examina-
tion of the strata and their fossils, assigned the “ Perna-beds,”
“‘ Atherfield clay,” and “ Crackers” of the Isle of Wight, and the
well-known “Couche rouge” of Wassy, in the Department of the
* Trans. Cambr. Phil. Soe. vol. ix.
+ Quart. Journ. Geol. Soc. vol. vi. p. 464 é¢ seq.
t Bull. de la Soc. Géol. de France, 2me sér. tome xii, p. 89.
R 2
224 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
Haute-Marne. Still later M. Lory showed that the relations
between the Rhodanien and the Urgonien were quite as close as
those between the former and the Aptien. As we thus appear to
have in the Rhodanien a complete link between the Upper and
Middle Neocomian, the boundary between these divisions becomes a
perfectly arbitrary one, and great diversity of opinion exists among
geologists to which of them certain deposits should be assigned.
Among those strata which lie upon the debatable confines of the
Upper and Middle Neocomian, we must class the Punfield Forma-
tion. But though there may be diversity of opinion as to the arti-
ficial scheme of classification best adapted for grouping these strata,
their true relative position in the Neocomian series is on palzon-
tological evidence perfectly clear. Ammonites Deshayesti, which
occurs in the Marine Band of Punfield, is a very widely distributed
species and has a restricted and well-defined vertical range, abound-
ing in the higher portions of the Neocomian, but being unknown
in the Urgonien or any lower bed. Vicarya Lujani and several
other of the Punfield shells are well-known and characteristic Rho-
damen forms. All the paleontological evidence points to the con-
fines of the Upper and Middle Neocomian as the true place of the
Punfield formation ; and it will, I think, be in accordance with the
views of a majority of the geologists of authority on this subject to
regard the “ Perna-beds” as the base of the Upper Neocomian, and
the Punfield beds as the highest part of the Middle Neocomian.
2. Coal-bearing Strata of Eastern Spain.—it is, however, in the
Spanish peninsula that we find the closest analogues of the Punfield
Formation. These beds have, during the last twenty years, been
made known to us by the admirable researches of MM. Vilanova,
de Verneuil, Collomb, de Loriére, and Coquand. As no description
of these beds has yet appeared in this country, it may be of interest
to notice briefly their chief features in this place. The recently
published very valuable memoir of M. Coquand enables us to do this
the more readily*,
The principal exposures of the deposits in question are situated
on the confines of the ancient kingdoms of Arragon and Valencia, in
the provinces of Teruel and Castellon de la Plana, though less im-
portant and outlying masses of the same strata occur in the valley
of the Guadalupe and in Catalonia, near the mouth of the Ebro.
In the province of Teruel, where they form three important pro-
ductive coal-basins, those of Utrillas, Gargallo, and of the Val
@Arino, the strata, which are more than 1600 feet thick, are
divisible into three series, which, however, pass into one another
* De Verneuil et Collomb. Bull. Soc. Géol. de France, 2° sér. tome x. (1853).
Vilanova, Memoria Geognostica (1859).
H. Coquand. Mém. de l’étage Aptien de l’Espagne (1865).
De Verneuil et De Loriére. Fossiles d’Utrillas (1868).
De Verneuil et Collomb. Carte géologique de |’Espagne et du Portugal
(Paris 1864). :
H. Coquand. Description géologique de la formation crétacée de la pro-
vince de Teruel. Bull. Soc. Géol. de France, 2me sér. tome xxiv. p. 144
(1868).
1871.] JUDD—PUNFIELD FORMATION. 225
by insensible gradations, and contain a considerable number of
fossils in common.
The lowest of these consists of alternations of limestones, sand-
stones, and marls, yielding a large series of fossils, by means of which
it is referred without doubt to the Urgonien. Its thickness is about
500 feet; and it rests indifferently (the Lower Neocomian being
absent) on all the older rocks. In the Utrillas basin this division
contains only jet, but in other districts it furnishes beds of coal. It
is in these that the mines of Santa Barbara and la Fuen Gargallo
are worked.
The second series, consisting of ferruginous sandstones and lime-
stones alternating with sandy clays, is that which contains the
same fossils as the Marine Band of Punfield. These beds, although
their fauna presents some peculiarities, are doubtless to be referred
to the highest portion of the Middle Neocomian. At Utrillas, where
they attain a thickness of 530 feet, they contain ten beds of coal,
lignite, or jet, which are extensively worked. Itis these beds which
constitute the Calcaire a Trigonies of M. de Verneuil. The fauna
of these beds seems to be especially characterized by the presence in
great abundance of Gasteropods of a new genus, which has already
unfortunately received four names (Cerithium, Omphalia, Cassiope,
and Vicarya). No less than six species of this genus have been
described from Utrillas, three of which occur at Punfield, and one
of them in the “ Rhodanien”’ of Switzerland. Itis remarkable that
there is scarcely a single fossil found in the Marine bed of Punfield
which does not also occur in these Spanish beds.
The third and highest of these series of Spanish rocks consists of
variegated and mottled clays and sands of bright colours (crimson,
grey, green, violet, and white), which greatly resemble the Keuper,
and were, indeed, long mistaken for it. They are probably in great
part of freshwater origin, though a few marine shells have been
found in them, which enable us to refer the series to the Upper
Neocomian. Their lower portion consists of dark-coloured clays
with a pyritous combustible mineral, formerly used for the manu-
facture of alum. This series, which is 600 feet thick, contains beds
of lignite, which are worked in many places. Itis overlain by strata
representing the Gault and other members of the Cretaceous.
These coal-basins of Eastern Spain have been estimated as being
capable of supplying the whole of the peninsula for more than 200
years.
VIII. Conctvston.
The grounds on which I have ventured to suggest that the strata,
the nature and relations of which I have endeavoured to illustrate
in the preceding pages, are worthy to rank as an independent for-
mation* are as follows :—
* The term “formation” is unfortunately employed by English geologists
with two very different significations—either to indicate great groups of strata
like the “Silurian” or “Jurassic,” or for smaller divisions, like the ‘‘ Ludlow
series,’ or the “Great Oolite.” It is with the latter meaning only I have
226 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 8,
1. They present very distinct mineralogical characters, separating
them alike from the overlying Neocomian and the subjacent Wealden
proper.
2. They are of considerable thickness, attainmg a maximum of
230 feet.
3. They present evidence of having been deposited under condi-
tions differing alike from those of the marine Neocomian above and
the purely freshwater Wealden below.
4. They yield a considerable marine fauna (between 30 and 40
species being already known), which is remarkably distinct and well
characterized.
5. They are the undoubted nanaetines of a formation which
in Spain attains to a vast thickness, and which, alike from its marked
paleontological characters and its great economic value, is of great
importance.
6. Their relations to the Wealden and Neocomian are precisely
analogous to those of the Purbeck formation to the Oolite and
Wealden ; and they are therefore equally deserving with it of a di-
stinctive title.
_ At the same time I have endeavoured to show that these beds
may be regarded indifferently either as the highest member of the
Wealden in our classification of the series of terrestrial strata, or as
a portion of the Neocomian in our grouping of the marine series.
The application to them of a distinctive name is therefore, although
a necessary, perhaps only a provisional expedient ; but the same is
to a greater or less extent true of most of our geological terms.
Discussion.
The Presipent remarked that the limited amount of freshwater
formations in this country was an obstacle to their correlation, and
stated that Constant Prévost had endeavoured to correlate the
Secondary freshwater and marine formations.
Mr. Gopwin-Avsten remarked upon the thinning out of the
Lower Greensand, especially in France, upon the imperfection of
our knowledge of the great Cretaceous formation, and upon the
probability of the intercalation of freshwater conditions in the
Lower Greensand. The formation at Punfield seemed to present an
intercalation of marine between purely freshwater conditions. He
indicated how a slight change of level might have intercalated ma-
rine conditions in the Wealden. ‘The deposition of the White Chalk
and Oolite occupied enormous periods (in both cases purely marine),
during which the northern hemisphere was a great northern ocean ;
and as the distribution of land and water was due to the operation
of great cosmical laws, the duration of terrestrial and of the inter-
mediate freshwater conditions was probably of equal length.
Mr. Erunriner observed that out of sixty or seventy species
employed the word in this paper, the term «“ system” being applied to the
greater groups of strata.
1871.] JUDD—PUNFIELD FORMATION. 227
from the deposits in Eastern Spain we have thirty-nine or forty in
Britain. The fauna was, indeed, precisely the same. He referred to
several of the species, and intimated his intention of describing and
figuring those forms which have not been.detected in the Spanish
deposits. ,
Mr. Szxtzy stated that he could not agree with Mr. Judd in his
conclusions, and that he objected to the method adopted by him..
He had examined all the sections, and was convinced that they
showed neither a physical nor a paleontological break, and that the
several beds could be so well traced that the base of the section
at Swanage was superior to that seen in the section at Brixton,
in the Isle of Wight. He identified the shell noticed as a Vicarya
asa Greensand form. There was nothing in the fossils to indicate a
separation from the Lower Greensand, of which he regarded these
beds paleontologically as forming a part. Hach division was to be
traced westwards continuously, but changing in mineral character.
Mr. Seeley objected to the correlation of these deposits with others
occurring in Spain or any other distant locality, and considered the
community of fossils not sufficient to establish such a correlation.
He objected also to the introduction of a new term into geological
nomenclature.
Mr. Jenxins remarked on the value of Mr. Judd’s description of
the sections, even if his deductions were to be rejected. He regarded
the establishment of a Punfield formation as unnecessary, and cited
the Purbeck and Portland beds as examples of analogous freshwater
and marine deposits. He indicated that the Weald may be regarded
as the freshwater equivalent of the Lower Neocomian. He doubted
whether the shell referred to Vicarya really belonged to that genus.
Ammonites Deshayesit was said to have a restricted range in time.
Mr. Jenkins remarked that it was very widely diffused, and there-
fore should have a wide range in time, which would invalidate the
argument founded on it.
The Rey. O. Fisnzr stated that in 1853 he had observed a fault
cutting off the Gault from the Punfield beds, and that its position
might account for the disappearance of a great mass of Lower
Greensand.
Mr. Jupp, in reply, said that he did not propose the term Punfield
formation as a definitive term, but only as a matter of convenience.
He believed that strata could be positively identified by the organic
remains contained in them, although the method may have been
grossly abused. Physical investigations alone led to nothing but
confusion, as might be seen by the stratigraphival attempts of the
predecessors of William Smith. The name Vicarya for the shell
which had been referred to was only provisionally adopted, on the
authority of De Verneuil and other writers.
228 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
2. Some Remarxs on the Denuparion of the Ooxrres of the Batu
District, with a THrory on the Denvpation oF OoxitsEs generally.
By W. SrepHen Mircretr, Esq., M.A., LL.B., F.G.8., of Gonville
and Caius College, Cambridge.
[Abridged.]
THE theory commonly held as to the origin of the Oolite hills of
this country is, that the strata of which they are composed were
originally deposited in sheets continuous over large areas, that the
valleys are entirely the result of denudation, which has left the
intervening masses standing out as hills, and that it is generally
possible to recognize on opposite sides of a valley at the different
horizons the individual beds which were formerly continuous across
that valley. The author believed that the following theory had
equal claims to credence :—
That the sedimentary deposits of any particular Oolitic district were
probably originally deposited in continuous beds, but that the lme-
stones im many instances probably never extended beyond the areas
they now occupy.
The object of the paper was to show that the Bath district was
one of these instances; and the following were the chief points
brought under the notice of the Society.
In the Bath district, while the beds of the Great Oolite lime-
stone are for the most part approximately horizontal over the pla-
teaux of the downs, they thin out at the edges of the hills. Mr.
Sanders in his map of the district has marked the few Oolite hills
which come within the map as everywhere dipping towards the
valleys.
There is no evidence here of a washing away of the underlying
Fuller’s Earth, and a consequent drop of the limestone, as is sug-
gested by Mr. Witchell to be the case in the Cotteswolds*. The
Fuller’s Earth might be scooped away for many feet under the
limestone before the latter would move. When it did move, it would
probably break off and slip or roll down the hill-slope. Here the
thinning out is the same when other beds of the limestone underlie ;
there is no displacement from the general mass. [It is just possible
that they may be cases of false bedding, with the layers that were
above them swept away; but the author could not see by what
agency this would be effected. |
To explain this thinning out, the probable origin of the beds was
taken into consideration.
I. The limestones.—The commonly received view that the material
of the Great and of the Inferior Oolite was accumulated by corals
was supported by quotations from Jukes’s ‘ Voyage of the Fly,’ and
Darwin’s ‘ Voyage of the Beagle.’ Recent coral-reefs are described
as consisting of “‘ rock fine-grained, only here and there exhibiting
any organic structure.” They show lamination and a jointed struc-
ture; and the bedding round the edges of an island dips towards the sea.
* Proceedings of the Cotteswold Nat. Club, 1867.
1871. ] MITCHELL—OOLITE-DENUDATION. 229
The structure of the rock varies, being compact, granular, or Oolitic
limestone, or loose calcareous sand. Many of these masses are de-
scribed as “‘ intersected by narrow channels of deep water.”
IJ. The sedimentary beds.—These were considered in reference to
the influence their accumulation would have on the accumulation
of the coral-masses. Many causes will from time to time change
both the rate of accumulation and the extent of the area over which
the sedimentary accumulation will take place. If such accumula-
tion take place in the same sea with coral-growth, a turbid condi-
tion of water may alternately encroach on and recede from the
coral-area. ‘These occasional irruptions would then temporarily in-
terfere with the coral-growth. In the case of the permanent en-
croachment of sediment on a district of coral islands and reefs, the
contour of the gradually depressed islands would be protected by the
sediment, which would also fill in the deep channels between them.
These considerations, it was suggested, may serve to explain the
“dip towards the valley” as mapped by Mr. Sanders, or “the
thinning out,” which is believed by the author to occur. The hills
were probably coral islands submerged, and covered up by sedi-
mentary matter. When the whole area, after subsequent elevation,
became subject to denudation, the yielding sedimentary matter being
swept away left the limestone islands standing as hills.
This naturally leads to the question whether the limestones them-
selves have suffered denudation. The author thought there can
have been but little, if any. He considered first the mechanical
action of water. He pointed out that the Great Oolite is traversed
by numerous vertical joints and fissures, which split it up into what
may be roughly termed cubical blocks. The surfaces of the joints
are generally covered with crystalline carbonate of lime. The rain
falling on the plateaux would at once percolate through the surface-
soil and “ heading,” and would pass off in the fissures. There would
thus be no accumulation of water, therefore no body of water in
motion, therefore no mechanical denudation. Elie de Beaumont’s
suggestion, set forth in 1843 in his ‘ Lecons de Géologie pratique,’ that
where there is no mechanical denudation, there must be accumula-
tion of vegetable soil, has not been objected to in principle, though
the extreme lengths to which he carried the idea have been attacked.
It is most probable that a protective covering of vegetable mould has
everywhere covered these Oolitic hills.
Secondly. With regard to chemical denudation, as each block is
bounded above and below by a parting of clay, and on its four sides
by crystalline carbonate of lime, the author could not see how
chemical denudation could take place except in an accidental way.
These remarks apply to the Great Oolite. The Inferior Oolite
in this district nowhere forms the summit of a hill; it is only to be
seen in sections on the sides of the hills. If it also was formed in
detached islands, some of the original edges of these islands may be
still hidden from our view by sedimentary matter preserved from denu-
dation by the Great Oolite above ; its origin must be dealt with in a
locality where it forms the tops of the hills. Itmay, however, happen
230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 8,
that the edges, or one of the edges, of an Inferior-Oolite island may
be coincident in position with a Great-Oolite island above.
There remains the question of the meaning of finding on opposite
sides of a valley zones containing assemblages of similar organic
remains. The author believed that this in no way bears on the
question of the original continuity or otherwise of the two sides.
If there are beneath the sea two spots (a and 6) near together,
having exactly similar conditions for life, the assemblage of forms
at both places might be the same, whether a and 6 are separated by
a channel or not.
In conclusion, the author remarked that, though he had arrived
at this idea inductively, yet he believed it would be fair to start
with the statement that coral islands when covered up would retain
their contour; and it would rest with those who insist on continuous
limestone-beds 7m all cases to show why the islands with deep
channels between them must have been broken up and spread out as
a continuous sheet before the sedimentary deposit was accumulated
on them. He also expressed his belief that the present view com-
monly held affords a correct explanation of the phenomena of Oolite
valleys in many cases.
Discussion.
Prof. Morris did not consider that the author’s views as to the
oolitic masses round Bath being originally isolated coral banks with
clay beds, although suggestive, were quite satisfactory. He pointed
out that the strata on each side the valleys were similar in structure,
mineral character, and fossil contents, and were once continuous ; and
the present intervening deep valleys were rather due to the movements
which the area had undergone in producing lines of weak resistance,
subsequently assisted by the erosive action of percolating and running
water, both in excavating and undermining the harder rocks, so as
to cause them to bend towards the hill-sides, or fall in larger or
smaller masses on their slopes.
Mr. Seetzey thought that Mr. Mitchell was justified in applying
considerations drawn from the formation of coral islands to the
elucidation of the phenomena under discussion. He maintained
that shallow-water limestones must always occur in isolated masses
with intervening masses of clay, and that the clay might be washed
out, leaving the limestone as hills.
Mr. Wuiraxker held that when like beds cropped out on the tops
or flanks of opposing hills it was a logical inference that the said
beds had once spread across the space between, and that there was no
need to call in the agency of supposed coral islands to explain the
occurrence of isolated masses of limestone, which were perfeetly
accounted for by denudation, an agency that involved no supposition,
and was quite equal to the work.
Mr. Eruerinet remarked that the mollusca of the outliers of the
Oolites in the Severn Valley were constant in beds at the same rela-
tive level. He also referred to the sliding of the oolitic strata of
the Cotteswolds upon the subjacent clays as accounting for the dip
1871.] TREVELYAN—LITHODOMOUS BORINGS. 231
towards the valleys mentioned by the author. He considered that
the valleys had been scooped out by denudation.
The PRESIDENT inquired whether the author was provided with
any sections showing the thinning-out of the beds.
Mr. Mrrcuett, in reply, stated that he had seen both sides of
what he regarded as coral reefs. He remarked that his hypothesis
had been arrived at by induction, but that the question might be put
strongly in a deductive form, by inferring from observations on ex-
isting coral reefs that those of the Oolites must have been covered up
as islands. He remarked that if the oolitic beds had slipped, as
described, upon the underlying clays, they could hardly range on
opposite sides of the valleys. He pointed out that the action of
water in covering the blocks of Oolite with crystallized carbonate of
lime would be protective, and remarked, in reply to Mr. Etheridge,
that the surface of the reefs whilst under water was virtually a sea-
bottom on which mollusca lived, so that their occurrence at corre-
sponding levels in different hills was not to be wondered at.
Frsrvary 22, 1871.
John Thornton Harrison, Esq., C.E., 3 Park Place Villas, Maida
Hill, and 1 Victoria Chambers, Westminster, and M. Hawkins
Johnson, Esq., 379 Euston Road, N.W., were elected Fellows of the
Society.
The following communications were read :—
1. On supposed Borings of LirHopomous Mottivusca. By Sir W. C.
TREVELYAN, Bart., M.A., F.R.S.E., F.S.A., F.G.S.
[ Abstract. ]
Tue author referred to Mr. Mackintosh’s paper on perforations sup-
posed to be made by lithodomous Mollusca* in the limestone of
Lancashire and elsewhere, and stated that from his examination of
specimens in the Society’s museum, and of examples of these per-
forations in situ, he was convinced that they are the work of some
of the common terrestrial Mollusca, as maintained by him long ago in
Jameson’s Edinburgh Journalt. He confirmed Mr. Jeffreys’s objec-
tion to the assumption that these perforations were made by marine
Mollusca, founded on the form of the perforations and their range in
height, and remarked that length of time is so essential an ele-
ment in their production that their formation is not likely to be
observed even in old quarries.
The author, in conclusion, referred to some remarks made by
Mr. Mackintosh f on the “terminal curvature of slaty lamine” ob-
* Quart. Journ. Geol. Soc. 1869, vol. xxv. p. 280 ; Geol. Mag. vol. iv. p. 295;
and ‘Scenery of England and Wales,’ pp. 288-398.
+ Vol. xl. p. 396.
+ Quart. Journ. Geol. Soc. 1867, vol. xxiii. p. 323.
232 PROCEEDINGS OF THE GEOLOGICAL society. _[ Feb. 22,
served by him in West Somersetshire in 1866, and stated that in
1849 he had himself called attention * to the marks of glacial action
shown in the terminal curvatures of slaty rocks in Forfarshire, and
suggested that they were to be explained by the progression of a
thick covering of ice along the edges of the slaty beds.
Discussion.
Mr. Gwyn Jerrreys read extracts from the Rev. Mr. Hodgson’s
‘History of Northumberland’ (published in 1827), in which these
borings in limestone were referred to the action of snails. Mr.
Jeffreys considered the foot to be the sole instrument employed by
the boring Mollusca in excavating their burrows. He exhibited
specimens of Lias from Lyme Regis perforated by Pholas, and of
hard limestone from Malta perforated by Lithodomus, and remarked,
in connexion with the notion that asperities on the shell might be
boring agents, that the shell of Lithodomus is perfectly smooth.
Prof. Ramsay mentioned that he had seen Helices taken out of
these holes at Tenby by Dr. Buckland, who believed that the snails
effected the perforations by the agency of an acid.
Mr. Cuarteswortn thought that if so much uncertainty could
prevail upon such a subject, it threw great doubt upon some of the
grandest generalizations of geology. He referred to the evidence
connected with the glaciation of the Great Orme’s Head, in which
the origin of the perforations under discussion was of much import-
ance, Mr. Darbishire maintaining that they were the work of Pho-
lades, while Mr. Bonney asserted that they were produced by snails.
In the same way the origin of the celebrated borings in the Temple
of Jupiter Serapis might be disputed, and the generalization founded
upon it rendered doubtful. Mr. Charlesworth noticed the necessarily
small proportion of borers to the whole snail-population of Britain,
and remarked especially upon the absence of perforations in the
chalk districts. He considered that repeated observations were ne-
cessary before this snail-engineering could be admitted, and sug-
gested a systematic course of experiments.
Mr. Borp Dawns suggested that the carbonic acid exhaled by
snails in respiration might act upon limestones, and remarked that
chalk weathers too rapidly to preserve the excavations,
2. On the probable Cause, Date, and Duration of the Guactat Erocu
of GroLoay. By Lieut.-Col. Drayson, R.A., F.R.A.S.
(Communicated by Alfred Tylor, Esq., F.G.S.)
[ Abstract. ]
Arter referring to the evidence of the occurrence of a Glacial
Epoch, and to the various hypotheses which have been proposed to
* Jameson’s Edinburgh Journal, vol. xlvi. p. 377.
1871.] DRAYSON—GLACIAL EPOCH. 233
account for it, the author brought forward the following considera-
tions :—
Of the three principal movements of the earth, namely its daily
rotation on its axis, its revolution round the sun, and the slow coni-
cal movement of its axis of rotation round the poles of the ecliptic,
the third is, in the author’s opinion, the cause of glacial epochs.
The angular distance of the pole of the ecliptic and the pole of the
heavens is at all times the exact measure of the obliquity of the
ecliptic, or the extent of the Arctic circle upon the earth. There is
evidence that during the last 2000 years these two poles have gra-
dually decreased their angular distance, so that, while the pole of the
heavens moves round some curve at the rate of about 1° in seventy-
two years, it approaches the pole of the ecliptic at a variable rate, at
present about 46” in a century. The author had calculated from
the recorded positions of the pole of the heavens during the last
2000 years, the curve traced by this pole with relation to the pole of
the ecliptic. He found it to be a circle, the centre of which is 6°
from the pole of the ecliptic, and 29° 25’ 47" from that of the hea-
vens.
Taking this curve as a guide, the author finds that 2000 years
ago the angular distance of the two poles was about 24°, giving a
climate scarcely different from that now prevailing. 4000 years
ago the angular distance would be about 29°, when the climates of
high northern and southern latitudes would present much greater
seasonal changes than at present; and these changes would go on
increasing back to the year 13,000 B.c., at which period the distance
between the two poles would be greatest, namely 35° 25' 47".
This would bring the arctic circle down to latitude 54° 35’ N., that
is to a line passing south of Moscow, just north of Berlin, north of
Amsterdam, nearly through the middle of Great Britain, and then
through Labrador and British Columbia. All the countries north of
these places would be subjected to arctic conditions ; and these would
prevail with even more severity than at present in the winter, whilst
from the greater elevation attained by the sun in summer that sea-
son would be much hotter than at present, the summer of the lower
arctic latitudes being even tropical in its intensity. These extreme
changes of climate would prevail, according to the author, during
a period of about 15,000 years; that is to say, commencing about
21,000 years ago, the climate would become more and more extreme
up to about 15,000 years ago, and then gradually more and more
equable to about 6000 years ago.
Discussion.
Prof. Ramsay inquired whether the author’s theory involved the
recurrence of glacial epochs, and whether he considered the course
of the described phenomena to be constant in early astronomical
epochs.
Rey. Osmonp FisHer inquired whether the curve was founded on
observed facts, or whether it was obtained from physical considera-
234 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 22,
tions. He also asked whether the line representing the change in
the direction of the pole formed a reentering curve, and whether
the theory would account for the climate of Greenland in Miocene
times. He suggested changes in the form of the earth which must
have affected the direction of its axis.
The Presipent remarked upon the difficulty that arose from
astronomical theories differing so much among themselves. He
referred particularly to Adhémar’s theory, and remarked that the
difficulty connected with it is, that it invokes a recurrent cause,
which must produce similar effects every 21,000 years, whilst there
is very little evidence of glacial action during the whole long period
of the Tertiary epoch.
The AvrHor, in reply, stated that he could not go back beyond
30,000 years, but that he thought glacial conditions must recur. He
had not astronomical data beyond 2500 years ; and these were very
vague. The motion would be the same in kind, but uncertain in
degree. His theory was based entirely upon observed facts. In
laying down the curve, he considered it safe to go as far as the semi-
circle, as he had observations covering 40°; but he could not say
whether the curve would be a reentering one, although it showed a
tendency that way, and would certainly be very nearly so. With
regard to the change of climate of Greenland, as evidenced by ita
Miocene flora, he was not sufficiently versed in botany to pronounce
an opinion. He remarked, in conclusion, that the distance of the
earth from the sun did not seem to affect the climate of the Southern
Hemisphere, and stated that Venus is at present suffering under a
most severe glacial epoch.
3. On AttopHaNE and an Attiep Minerat found at NortHaMpPTon.
By W. Dovetas Herman, Hsq., Student of the Royal College of
Chemistry.
(Communicated by W. W. Smyth, Esq., F.R.S., V.P.G.S.)
THE only English localities at which, to my knowledge, allophane
has been shown to occur are the chalk-pits at Charlton, near Wool-
wich, the Purley downs, near Croydon, and a spot not far from
Tavistock, in Devonshire. Dr. Charles Berrill, however, shortly
before his death, discovered a mineral much resembling the Charlton
allophane in physical properties in a pit opened in the ironstones of
the Northampton Sand (beds of Inferior-Oolite age) in the grounds
of the Northampton General Lunatic Asylum. It occurs as an amor-
phous, translucent, somewhat hard and exceedingly brittle mineral,
of a yellowish colour inclining to red, and incrusting the surface of
a sandstone rock.
The following analyses of a specimen of this mineral presented by
Mr. Sharp, of Dallington, to the Museum of Practical Geology fully
bear out, I think, its claim to be called allophane. I append, for
the sake of comparison, Mr. A. B. Northcote’s analysis of a charac-
teristic sample from Charlton.
1871.] HERMAN—ALLOPHANE. 235
Northampton.
pees -~\ Charlton.
I II. Mean.
Water expelled at 100° C. 24°70 24:88 24-80 27°11
» fixedat 100°C. 1454 14:54 14-54 15°80
SiO, 23°09 22°92 23°01 20:50
Al, O, 31:24 31-42 31:33 31:34
Fe, O, 2°35 2:18 PAPAS a aN CPB
OOO ROT GSE er eo aint: SoBe) Ny Cem eI Moe 31
CaO 2°51 2°48 2°49 1-92
MgO ‘01 01 SON PN
(Normal) ...... Co, 1:28 1:28 1:28 1-69
(Aisibicarbonate)|\ COR sei ecscn wie Pict crilay iy Veer 1:04
99°72 99°71 99°72 99°71
In these analyses the amount of carbonic acid was deducted from
theloss on ignition; and in Mr. Northcote’s case, in addition, the
carbonic acid existing as bicarbonate was deducted from the loss at
100° C.
The excess of silica in the Northampton specimen is probably due
to an almost unavoidable admixture of sandstone, upon which the
allophane formed an incrustation.
Mr. Sharp, in a paper lately read before the Geological Society of
London, and published in the Quarterly Journal of the Society,
vol. xxvi. p. 367, speaking of a section of the Northampton Sand in
the grounds of the Northampton Lunatic Asylum, remarks :—
«< One set of joints in this section have a direction N.W. and 8.E. ;
and the crevices are frequently filled with a soft white material,
which, upon analysis by the recently deceased Dr. Berrill (formerly
a student at the Royal School of Mines), was shown to be allied to
allophane.”
The substance here alluded to, a dull, whitish, pulverulent, earthy
mineral, that may be polished by the nail, adhering strongly to the
tongue, and exhibiting no trace of crystalline structure under the
microscope, is by no means rare in many localities both in the iron-
stones and limestones of the Inferior Oolite of the Midland Counties.
Professor Morris, in his paper on the allophane of Charlton*,
apparently alludes to a similar mineral. He says :—During the im-
portant investigations (under the direction of Dr. Percy, at the School
of Mines) into the chemical composition of the different iron-ores of
Britain, a white powder (probably pholerite) was observed associated
with some of the clay-ironstone ; the following is its analysis by Mr.
Dick :—
41-78
36°99 -
* Quart. Journ. Geol. Soe. vol. xiii. (1857) p. 15.
236 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 22,
“‘T have also collected a similar mineral substance occurring on the
surface and filling the crevices of the white oolite of Lincolnshire,
where this rock is covered by the soft shales, sandstones, and clays
belonging to this series. It has probably originated in the same
manner as scarbroite and allophane, by the decomposition of some
of the mineral substances of the overlying strata.”
No analysis is given of this mineral ; but, from its geological posi-
tion and mode of occurrence, it resembles the earthy substance found
by Dr. Berrill in the Northampton Sand, although this last, as will
be seen from the following tabulated analyses, agrees much more
nearly in composition with halloysite or samoite than with pholerite.
Name. Locality. | SiO,. |Al, O,.) H, O. Analyst.
Pholerite ............ Fins. 41-65 | 43°35| 15:00} —_....2e.eeave Guillemin.
Ty ni. eocneaeceee Darlaston. | 41:78} 36:99| 14-26 |Fe, O, 4-51, MgO Dick.
0:16, Ca 0-48.
SSENETVOTLNS) Goansonopoossnd! = Gabecn 31:25 | 37°21 | 30:45 |MgO 06, NaO -06,} Silliman.
CaCO, ‘01.
3 en Ake Mee 35°14} 31:95 | 30°80 |MgO 1:05, NaO 3
trace, CaCO, 1-21.
Halloysite .........-.. Anglar. 39°50 | 34:00} 26°50] —.... ..seonvee Berthier.
(dried at 100° C.) e 44-94| 39:06] 16°00] _.....2..- “0
EKarthy mineral...... Northampton.| 35°19 | 32:22} 29-87 |Fe,O,-02, FeO-28,| The Author.
CaO 1:72, MgO
03, CO, 39,
SO, trace.
(dried at 100° C.) = 43°92 | 40:22] 15°86) —....... sn 0 a
In the analysis of the earthy mineral from Northampton the loss
due to the expulsion of carbonic acid was deducted from the loss on
ignition, and the increase in weight arising from the oxidation of
the ferrous oxide was added to the water fixed at 100° C.
On the supposition that the mineral consists essentially of water
fixed at 100° C., silica, and alumina, it would be represented by the
formula
8 Al, 0, 15810,+-18H, 0;
but if the water that is given off at 100° be considered essential to
its composition, it would be expressed by
Al, 0, 28i0, +5H,0.
The mineral dried at 100° is exceedingly hygroscopic, speedily re-
gaining almost the whole of the water it had lost, and that too in
well-ground, tightly fitting watch-glasses.
Discussion.
Mr. Davin Forszs stated that he had found phosphoric acid in the
first-mentioned mineral, which was perhaps the cause of its lustre.
The mineral was probably not pure allophane.
Prof. Morris suggested a chemical and microscopical examination
1871. ] HAWKSHAW—PEAT-BEDS, HULL. 237
of the strata above the places in which these minerals occur, which
would probably reveal the conditions under which they had been
formed. They were probably produced by the decomposition of sili-
cates in the overlying rocks during the percolation of water. This
applies also to the Charlton locality. i
Mr. CarrurHers mentioned that allophane often fills the inflo-
rescence of the Cycads of the Yorkshire Oolite, entirely destroying
the vegetable structure, and that it also occurs in clay nodules from
the coal-measures. Mr. Carruthers suggested that the decomposi-
tion of vegetable matter in clays might aid in the production of the
mineral,
4. Notes on the Peat and Unprrtyine Beps opseRveD in the Con-
strucTION of the AuBERT Docx, Hutt. By J. C. Hawxsnaw,
Ksq., F.G.S.
[Abridged.]
Tue author described the Albert Dock as extending east and west
along the foreshore of the Humber at Hull, for a distance of 4000
feet. The total area excavated was about 30 acres. All the exca-
vations were carried to a depth of at least 8 feet, and in some in-
stances of 27 feet, below the level of low water.
Before the commencement of the excavations the Hessle Clay,
peat, and overlying silt were met with in succession on the fore-
shore, the level of the top of the peat-bed at the west end of the
area being about 3 feet above the level of low water, and its thick-
ness from 3 to 4 feet. Eastward the bed followed the undulations
of the clay without much variation in general level for half a mile,
when it began to dip, attaining a depth of 12 feet below low-water
level at the lock-entrance, and then rising again. From this depres-
sion of the peat-bed, and the appearance of the overlying silts, the
author thought it probable that this had been an old channel of the
river Hull, and that the upper part of the peat had been removed
by scour. In support of this view he quoted the statements of
antiquarian writers.
The peat rested directly on the Hessle clay, into which roots pene-
trated to a distance of 5 or 6 feet, generally following the direction
of vertical joints, which gave the clay a tendency to split into
prisms. These joints did not occur in the Purple Clay; and the author
suggested that they may have been caused in the Hessle Clay by its
drying by exposure before becoming covered with vegetation. The
sides of the joints were grey ; and this colour pervaded all the clay
that was intermixed with the peat and extended for a distance of
from 1 to 2 feet into the overlying beds of silt. This grey tint pro-
bably resulted from the decoloration of the iron, due to deoxidation
by the vegetable matter of the peat.
At its highest level, at the west end of the dock, the peat consisted
almost entirely of vegetable matters, including large accumulations
of moss, leaves, and masses of brushwood, layers of oak-leaves with
acorns, hazel-nuts, and fir-cones. Numerous remains of Coleoptera,
VOL. XXVII.—PART I. s
238 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 22,
chiefly wing-cases, were found. Trunks of oak trees, some of them
60 feet long, were scattered through the peat, and had evidently
fallen where they grew; and from the characters presented by most
of them, it would appear that they had grown close together. In this
part of the bed, at the level of low water, and beneath a thick layer
of moss, the remains of a fire were found. The author suggested
that, from the small extent occupied by the remains of this fire, it
was probably the result of human agency, as, if it had originated by
lightning or by the friction of dry branches, it could hardly have
been confined to so small an area.
The author inferred that no great change in the relative levels of
different parts of the bed has occurred, because at the lowest eastern
part the peat had been formed under water, branches and trunks of
trees being imbedded in a stratum of grey clay, the wood being
much of the same colour as the clay. In one large oak, 5 feet in
diameter, there was a hole filled with acorns and hazel-nuts, many
of the latter broken open at the end. This the author regarded as
the store of a squirrel, and he remarked upon its being the sole
trace extant of the existence of squirrels in the forests from which
this peat was formed.
With regard to changes of level, the author stated that, whilst in
other places an upward movement has been indicated*, the area ex-
amined seems to furnish evidence only of depression. Thus the sur-
face of the peat in the supposed old channel of the river Hull is 12
feet below the level of low water, whilst the bed of the present
river at South Bridge is only 6 feet below that level. The depres-
sion of the forest converted the land on which it grew into a marsh,
where soft vegetable matter accumulated rapidly and soon covered
‘up the fallen trees, the soundness of the timber indicating no long ex-
posure to the weather. As the land continued to subside, the marsh
was invaded by the waters of a tidal estuary, in which the Mollusca
lived whose shells occur in the grey clay overlying the peat, and
even in the peat itself. Of these the following forms occur:—
Scrobicularia piperata, Cardium edule, Tellina solidula, Hydrobia sp.,
and Bullina obtusa, all, except the last, in great abundance.
The arrangement of the trees at the east end of the dock was not
such as to indicate that they had been deposited in a current having
a constant flow in one direction. The bands of blue clay were
bulged out above as well as below the logs; and the author accounted
for this by assuming that the logs did not yield to compression like
the peat, from which, he thinks, an index of the compressibility of
peat might be obtained.
Among the sections accompanying this account, two differ, in
showing the Hessle Sand to thin out at the west end of the dock,
from the section published in the Society’s ‘ Proceedings ’+. When
the latter section was made, the excavations for the dock were not
completed, and the sand underlying the silt in borings westward
a Quart. Journ. Geol. Soc. vol. xxiv. p. 157.
-+ Quart. Journ. Geol. Soe. vol. xxiy. P 182, fig. 14.
t
1871.] HAWKSHAW—PEAT-BEDS, HULL. 239
“Was supposed to be a continuation of the Hessle bed, whereas the
excavations and subsequent borings showed that the Hessle Sand
thinned out at the west end of the dock. To the westward of the
west end of the dock the peat, Hessle Clay, and Hessle Sand have
been removed by the scour of the Humber down to the surface of
the Purple Clay, and the more modern deposits of Humber sand
and silt repose directly on the latter. In the section in vol. xxiv. of
the Society’s ‘ Proceedings,’ above referred to, the lower part of this
silt deposit, described as sand in the borings, is, in the writer’s
opinion, wrongly shown as a continuation of the Hessle-Sand bed.
Several borings were made in the foundation for the dock-wall
towards the west end of the dock; the thin bed of Hessle Sand
reached by these borings was similar in colour to that found
at the east end of the dock, where the Hessle Sand also thins
out. As the bed diminished in thickness it became similar in
colour to the adjoining clays. Good sections, about 500 fect in
length, of the junction of the two clays with the Hessle Sand, the
latter reduced to a thickness varying from 24 feet to 5 inches,
were exposed in the excavations for the foundations of the lock
at the east end of the dock, which were carried down to the
surface of the Purple Clay. Throughout those sections the sand
was nowhere absent, and the junction with the two clays was very
distinct. Where the bed was thick the sand was of a bright yellow
colour, much cross-bedded, and composed of fine rounded grains of
quartz, mixed with a considerable proportion of grains of chalk.
This Hessle sand was probably reconstructed out of the Purple Clay
in the same manner that the Hessle sand and gravel at Kelsey Hill
have, in Mr. Prestwich’s opinion, been reconstructed out of the
boulder clays. Two sections, each about 1000 feet in length, show
accurately the junction of the Hessle Sand and the Purple Clay.
There was no intermingling of the sand and clay. The Hessle Sand
was removed from the surface of the Purple Clay for the foundation
of the dock-walls, for a width of 30 feet along the lines of these
sections. ‘The appearance of the surface of the Purple Clay shows
it to have been consolidated before the deposition of the sand. A
depression about 6 feet in depth, and apparently due to erosion,
crossed the section at right angles. On one side the clay formed a
steep face; and the bottom of the hollow was strewed with small
gravel and scratched and rolled stones. Sometimes boulders were
found on the surface of this clay too large to be removed by the
current which probably swept the surface of the clay before the
deposition of the Hessle Sand.
The borings taken at the east end of the lock showed the purple
clay to be very compact, and free from stones and pot-holes ; these
borings were taken to ascertain the source of some springs which
burst out in the foundations before the excavations were completed.
With one exception, they extended to a depth of 58 feet below high
water, nothing but the solid clay being met with below the surface
of the Purple Clay. The water from the springs was brackish, and
was in all cases charged with from 2 to 5 per cent. of reddish-yel-
8 2
240 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 22,
low sand; the flow from one spring amounted sometimes to 1500
gallons per minute. For a long time their source was a complete
puzzle, as it was not suspected that water could find a passage
through the thick bed of Purple Clay. On a boring being made
through the Purple Clay, it was proved that the springs had their
origin in the lower sand-bed overlying the Chalk ; and it is most pro-
bable that the water found its way to the surface through the holes
of old borings made through the Purple Clay before the work was
begun. Several old bore-holes were found, during the course of the
excavation, filled with small pieces of chalk.
This bed of sand overlying the Chalk appears to be of some extent
in the neighbourhood of Hull. It was 16 feet in thickness where
a boring passed through it at the east end of the lock; and the
same sand was found by all the borings to the westward which
passed through the Purple Clay. It appears to increase in thickness
to the east of Hull, as a boring* taken at Blockhouse Mill shows a
thickness of 26 feet of sand between the Purple Clay and Chalk.
Several thousand yards of this sand were brought to the surface by
the springs in the lock; it was of redder colour than the Hessle
Sand, but contained, like it, particles of chalk.
Discussion.
The Presipent remarked upon the singularity of the occurrence of
a bed of ashes at such a depth in these deposits.
Mr. Gwyn Jzurrreys referred to the President’s paper on the
Kelsey-Hill beds, and remarked on some of the Mollusca obtained
by Mr. Hawkshaw.
Mr. Boyp Dawxrns mentioned the occurrence of a submarine
forest on the coast of Somersetshire, forming a layer of peat, beneath
which was a land-surface, on which the forest had grown, and in
which flint-flakes were found at Portlock and Watchet on digging
through the peat. He remarked on the depression of the coast of
Somersetshire within the human period, and suggested that the
forest at Hull may have been contemporaneous with that of Somer-
setshire.
Prof. Morris inquired whether any trees or roots were found as
when growing. The shells obtained were estuarine. Prof. Morris
remarked on a submerged forest near Whittlesey, with terrestrial
plants and freshwater shells imbedded in the overlying clay.
The Avrnor, in reply, stated that the trees had fallen where they
grew. No direct evidence of man’s presence had been found in con-
nexion with the remains of the fire; but judging from the general
appearance of these remains, he could come to no other conclusion
than that the fire was the work of man.
* Phillips’s ‘Geology of Yorkshire,’ second edition, p. 27.
1871.] RAMSAY—PRETRIASSIC RED ROCKS. 241
Marca 8, 1871.
Lieut. Lewis de Teissier Prevost, H. M. 47th Regiment, and John
Haines, Esq., Vernon Lodge, Addison Road, Kensington, were elected
Fellows of the Society; and Dr. C. Nilsson, of Lund, was elected
a Foreign Member of the Society.
The following communication was read :—
On the Rep Rocks of Enetann of older date than the Trias.
By A.C. Ramsay, LL.D., F.R.S.
In a previous paper* I stated that the red colour which stains the
New Red sandstone and marl is due to the presence of peroxide of
iron, the iron probably having found its way into the water as a
carbonate, which by contact with the air, afterwards became perox-
idized, and encrusted the sedimentary grains as a thin pellicle. I
further stated that I believed that iron could not have been depo-
sited in this manner in an open sea, but rather in inland isolated
waters, and I confirmed this opinion by other facts which tended
to prove that our New Red strata were formed in a lake or lakes,
which at the period of the deposition of the Keuper marls, were
salt.
I now propose to examine the bearing of the red colour due to
peroxide of iron in other formations of older date, as to the physical
conditions under which those strata were deposited—that is to say,
whether they were formed in the open sea or in inland waters. In
doing this I will also take into consideration any other circumstances,
physical or paleontological, that may tend either to confirm or to
throw doubt on the idea stated above. I will not treat of the pre-
triassic red rocks either in ascending or descending stratigraphical
order, but simply in the manner that seems most convenient to illus-
trate the points at issue. If some of the following passages appear
like a partial repetition of arguments used in my previous paper, I
can only say that they are brief, and seem to me to be necessary for
the proper understanding of the questions I am about to raise.
Old Red Sandstone-—Mr. Godwin-Austen long ago stated his
opinion that the Old Red Sandstone, as distinct from the Devonian
rocks, was of lacustrine origin. The absence of marine shells helps
to this conclusion ; and there is nothing to indicate that the fossil
fish found in it belonged entirely to marine genera and species. The
reverse is the case; for the Polypterus, the nearest living analogue of
some of them, inhabits the rivers of Africa, and the Lepidosteus, less
closely allied, is found in the fresh waters of the North American
continent. Even though some Old-Red-Sandstone fish have been
found in the Devonian rocks of Devonshire and Russia along with
marine shells, this proves nothing except that some of them were
fitted to live in either fresh or salt water, like various modern fishes.
The Upper Silurian rocks of Shropshire, Herefordshire, Mon-
* On the Physical Relations of the New Red Marl, Rhztic Beds, and Lower
Lias (see p. 190).
242 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 8,
mouthshire, and South Wales are succeeded immediately by Old Red
sandstones and marls; and there is no visible unconformity between
them. Occasionally the Silurian rocks are red near the junction
with the Old Red Sandstone, as, for example, near Usk, and on the
banks of the Sawdde, near Llangadoc, in Carmarthenshire; but this I
regard as due to subsequent infiltration from above having stained
the strata. Colouring of this kind is by no means uncommon.
Thus the Carboniferous Limestone of North Lancashire, which
contains hematite, is overlain by red Permian sandstone, and both
the redness of the limestone and the ironstone itself are consi-
dered by Sir Roderick Murchison to be due to infiltration from above.
Coal-measure sandstones and shales, when immediately underlying
red Permian marls and sandstones, are frequently exceedingly red ;
and the same is the case with Carboniferous strata underlying the
Magnesian Limestone. The last Mr. Ward attributes either to “ the
action of carbonated water from the limestone above filtering through
porous grits and sandstones, and converting the protoxides contained
in them into sesquioxides, or by iron being brought from the over-
lying limstone, in the form of hydrate and carbonate, and rede-
posited in the rocks below”’*. (The Magnesian-Limestone soil is
always red, and I consider Mr. Ward’s last explanation the most
probable.)
The life of the Upper Silurian deposits in Wales, Shropshire, and
the adjoining counties continued in full force right up as far as the
narrow belt of passage-beds which marks the change from Silurian
muddy sands into lower Old Red Sandstone; and this abundance
of life is quite irrespective of the occasional red colour of the
uppermost Silurian rocks. In the transition beds, on the contrary,
genera, species, and often individuals are generally few in number
and often dwarfed in form, with the exception, perhaps, of part of
the Tilestone, near Llandovery and elsewhere in Carmarthenshire,
and a few other places. The more common genera are Anodontop-
sis and Modiolopsis of various species, Orthonota angulifera, Cucul-
lella antiqua, Grammysia extrasulcata, various species of Ctenodonta,
and some small univalves of the generaMurchisonia, Holopella, Turbo,
and Turritella. At Kington and south of Builth, where true pas-
sage-beds occur, the fossils are far less numerous, and almost all
of small size, including species of Modiolopsis and Modiola, Lin-
gula cornea, Platyschisma helicites, a small Discina, and a small
Theca, a few small Crustacea, Leperditia, Cytherellina siliqua, and
certain undetermined species. In some districts, as, for mstance,
at Ludlow and near May Hill, the very uppermost Silurian strata
also contain seeds of Lycopodiacez, and various fragments of unde-
termined land plants.
The land plants clearly indicate the neighbourhood of land; and
the poverty of numbers, and small size of the shells, a change of
conditions in the nature of the waters in which they lived.
The fish-remains found in the passage beds, and in the very base
* “On Beds of supposed othliegende Age, near Knaresborough,” by J. Clif-
ton Ward (Quart. Journ. Geol. Soc. 1869, vol. xxv. p. 291).
1871.) RAMSAY—PRETRIASSIC RED ROCKS. 243
of the Old Red strata, in which there are no Mollusca, are species of
Auchenaspis, Onchus (2 species), Pteraspis, Cephalaspis, and Plec-
trodus. These also in the main indicate a change of conditions,
which were, I believe, of a geographical kind.
The Kurypteride and Pterygoti in England almost entirely belong
to the passage-beds ; and one, Hurypterus Symondsw, is only found
in the lower Old Red strata.
The circumstances which marked the passage of the uppermost
Silurian rocks into Old Red Sandstone seem to me to have been the
following :—First, a shallowing of the sea, followed by a gradual
alteration in the physical geography of the district, so that the area
became changed into a series of mingled fresh and brackish lagoons,
which finally, by continued terrestrial changes were converted into
a great freshwater lake, or, if we take the whole of Britain and lands
beyond, into a series of lakes; and the occurrence of a very few
genera or even species of fish and Crustacea, common both to the
fresh and the brackish or even salt waters, does not prove that the
Old Red Sandstone is truly marine. At the present day animals
that are commonly supposed to be essentially marine, are occa-
sionally found inhabiting fresh water. Thus I am informed by
Mr. Murray, of the Geological Survey of Canada, that in the inland
fresh lakes of Newfoundland seals are common. They breed there
freely, and never visit the sea. The same is the case in Lake Baikal,
in Central Asia ; and though these facts bear but slightly on my pre-
sent subject, seals being air-breathing Mammalia, yet in some of
the lakes of Sweden it is said that marine Crustacea are found.
This may be accounted for in the same way that I now attempt to
account for these peculiarities in the Old Red Sandstone strata.
These Swedish lakes were submerged during the Glacial period ;
and being deep basins (scooped out it matters not by what pro- |
cess), while the land was emerging, and after its final emergence,
the salt water of the lakes freshened so slowly, that some of the
creatures inhabiting it had time by degrees to adjust themselves to
new and abnormal conditions*.
Again, we may suppose a set of circumstances such as the follow-
ing:—If by changes of physical geography of a continental kind
a portion of the Silurian sea got isolated from the main ocean, more
or less like the Caspian and the Black Sea, then the ordinary marine
conditions of the “‘ passage beds,” accompanied by some of the life
of the period, might be maintained for what, in common language,
seems to us along time. The Black Sea was once united to the
Caspian, the two together forming one great brackish lake. The
Black Sea is now steadily freshening ; and it is easy to conceive that
by the closing of the Bosphorus (a comparatively small geographical
change) it might be again converted into a fresh lake. At present
a great body of salt water is constantly being poured out through the
Bosphorus, and its place taken by the fresh water of rivers. At pre-
* For much important information on this subject, see Annals and Mag. of
Nat. Hist., 3rd series, vol. i. 1858, p. 50, “On the Occurrence of Marine Animal
Forms in Fresh Water,” by Dr. H. von Martens. Translated by Mr. W.S. Dallas.
244 PROCEEDINGS Ol THE GEOLOGICAL SCCIETY. [ Mar. 8,
sent, owing to the uncongenial quality of the water, many of the
Black-sea shells are strangely distorted, as shown by Edward Forbes.
Or if we take the Caspian alone, as it now stands, as an example,
we have a salt inland sea which, according to accepted views, was
once united to the North Sea and, possibly, at the same time to the
Black Sea, as shown by the Aralo-Caspian deposits, at a time when the
Bosphorus was still closed. Changes in physical geography have
taken place of such a nature that the Caspian is now disunited from
the ocean, while its waters are still inhabited by a poor and dwarfed
marine molluscan fauna, and by seals. If by increase of rainfall the
Caspian became freshened, evaporation not being equal to supply, it
would by and by, after reaching the point of overflow, be converted
into a great freshwater lake, larger in extent than the whole area
now occupied by the Old Red Sandstone of Europe*. It is even
conceivable that the great area of inland drainage of Central Asia,
now holding many salt lakes, might in the same manner be so changed
that all its lakes would become fresh and widened in extent, thus
occupying areas many times as large in extent as all the known
Kuropean Old Red Sandstone. Under these circumstances, in the
Caspian area we should have a passage more or less gradual from
marine to freshwater conditions, such as I conceive to have marked
the advent of the Old Red Sandstone. When the whole area was
fairly isolated from the sea, the sediments might by degrees get
into a condition to be coloured red in the manner previously men-
tioned. We have a case in point in an old inland sheet of water, as
shown by the red marls of the Miocene lakes of Central France. In
certain of the strata of the Old Red Sandstone, especially in the upper
beds, the colour has been here and there discharged in irregular
patches, probably through the reducing action of organie matter,
and the percolation of water containing carbonic acid.
Mr. Jukes divided the Old Red Sandstone of Ireland into two
portions. The lower series is conformable with and adheres to the
Upper Silurian strata. The upper series lies quite unconformably
on the lower, and adheres to and is conformable with the Carboni-
ferous strata. In Wales and the adjoining counties no such uneon-
formity has been clearly made out and mapped, though Sir Henry
De la Beche pointed out that such a division may exist, as shown by
the overlap of the upper strata across the lower, proceeding west-
ward from Breconshire into Carmarthenshire and Pembrokeshire.
However this may be, the thickness of the Old Red Sandstone is
often very great; and this to some minds, taken perhaps in conjunc-
tion with unconformity, may present a difficulty to the acceptance
of my view. In South Wales and Herefordshire the formation is
from 2000 to 7000 or 8000 feet thick, as determined by my mea-
surements carefully levelled in 1843. But on consideration these
circumstances do not appear to present any real difficulty. Ifthe great
hollow in which the Dead Sea lies were gradually to get filled
with fresh water and silted up, 1300 feet would be added above the
level of the present surface, without taking into account the depth
* Exclusive of marine Devonian rocks.
ees fale, RAMSAY—PRETRIASSIC RED ROCKS. 245
of the sea and the deposits that have already been formed; and the
upper strata all round would overlap the lower, apparently much
as the Old Red Sandstone strata do in Wales and the adjoining
counties. If the Caspian and other parts of the Asiatic area of
inland drainage got filled with fresh water, the same general results
would follow.
Neither does the unconformity mentioned by Mr. Jukes present
any insuperable difficulty, assuming his Lower Old Red Sandstone
to be represented in England and Scotland, of which as yet there is
no absolute proof. It indicates only great disturbance and denuda-
tion, while the red colour, and the total absence of fossils till we
reach the very uppermost beds of the Upper Old Red Sandstone,
point to inland waters. These fossils, itis well known, are terrestrial
ferns, Adiantites (Paleopteris) hibernicus, and a freshwater shell,
Anodon Jukeswi, together with the fish Glyptolepis.
Permian strata—I will now proceed to discuss the conditions
under which the British Permian strata were deposited. These, it
is well known, are usually divided in descending order into Mag-
nesian Limestone or Zechstein, with subordinate Marl-slate or
Kupferschiefer, and Rothliegende ; and though this division is
very convenient for great part of the Continent, it is not with
certainty perfectly applicable to the whole of England and some
other parts of Europe. If we take the whole country from near
Nottingham to Tynemouth, there is no marked line of division
between the Marl-slate andthe Magnesian Limestone ; and all along
that range the red rocks on which the limestone series rests are now
proved to be Carboniferous sandstones and shales stained by infiltra-
tion from above, which thus put on the likeness of Permian marls *.
The supposed Rothliegende has, indeed, almost disappeared from the
entire area.
The Permian marls, sandstones, conglomerates, and subangular
breccias of Leicestershire, Warwickshire, South Staffordshire, Shrop-
shire, and North Wales are as a rule all red, and have no visible
connexion with the Magnesian Limestone. In Lancashire, in upper
Permian strata, thin beds of magnesian limestone are interstratitied
with red marls; and these limestones, as Mr. Binney and Mr. Hull
state, may represent in time, as they do lithologically, the limestone
series in the east and north of England. The latter are also inter-
stratified with two or three occasional bands of red marl, while in
Lancashire the limestones have many marl-beds intermingled with,
and also both above and below them. Underneath the limestones
and marls of Lancashire there are soft red sandstones, of great thick-
ness, generally believed to represent the Rothliegende.
The Permian sandstones on the south and west coasts of the Cum-
brian country are red, as are those in the Vale of Eden. In the Vale
of Eden the Brockram at and near the base has no connexion with
* The Yellow sands at the base of the limestone beds are generally a residue
of sand. ‘The limestone, which is often sandy, rests on shale, which is compara-
tively impermeable to water. The limestone dips east; the carbonate of lime
has been carried away in solution as bicarbonate; and the sand remains.
246 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 8,
the Magnesian Limestone, and has been formed in quite a different
manner. It is a great brecciated conglomerate composed of angular
fragments of Carboniferous Limestone, cemented together by ecar-
bonate of lime, and as hard and solid as the Carboniferous Limestone
itself. In South Staffordshire, North Staffordshire, Shropshire, on
the borders of Wales and elsewhere the Permian strata have the
same general characters as those of parts of South Staffordshire and
Warwickshire, and consist chiefly of red sandstones and marls with
occasional brecciated conglomerates, which I have elsewhere de-
scribed.
I have given this brief sketch of the distribution and lithological
characters of the Permian strata of England, simply to remind my
readers of their general nature in various areas, and not because I
have any occasion to discuss in this paper any questions connected
with equivalent geological horizons of Permian age, or of the dis-
turbances that preceded the deposition of the Permian strata and
may have helped to rule their characters.
As with the New Red Marl mentioned in a previous paper*, so I
consider that the red colouring-matter of the Permian sandstones and
marls is due to carbonate of iron introduced into the waters, and
afterwards precipitated as peroxide in the manner previously stated,
and for the same reason, that I know none of the great formations
of British rocks proved by fossils to be formed of ordinary marine
sediment that possess this red colour except those that have been
stained from above by accident. I believe, therefore, that in this
circumstance alone we have an indication that these red Permian
strata were deposited in inland waters unconnected with the main
ocean, which waters may have been salt or fresh, as the case may be.
What other circumstances are there that more or less pear on this
question ?
First, as regards the plants of the British area, they are land-
species, and chiefly of genera common in the Coal-measures, viz.
Calamites, Lepidodendron, Walchia, Chondrites, Ullmannia, Cardio-
carpon, Alethopteris, Sphenopteris, Neuropteris t, and many frag-
ments of coniferous (?) wood of undetermined genera. These last are
occasionally met with in the Permian red beds of many parts of
England, generally silicified ; and inland waters would be likely to
receive fragments of land-plants borne into them by rivers.
This, however, forms no conclusive evidence, since land-plants are
not uncommon in the Lias and Oolites.
No Mollusca have yet been found in the red beds of Warwickshire,
Staffordshire, Shropshire, Wales, or the Vale of Eden, with the
exception of two or three casts of a brachiopod allied to Strophalosia,
found by Mr. Gibbs and myself in red sandstones near Exhall, in
Warwickshire ; and these occur along with Calamites and other land-
plants. In Lancashire, however, near Manchester, Schizodus was
found by Mr. Binney plentifully in Upper Red Permian marls, in
* On the Physical Relations of the New Red Marl, Rhetic beds, and Lower
Lias (supra, p. 190).
+ Taken from Mr. Htheridge’s lists.
1871. ] RAMSAY—PRETRIASSIC RED ROCKS. 247
strata sometimes associated with bands of fossiliferous magnesian
limestone. No shells of any kind have been found in the so-called
Rothliegende of Lancashire, or in the Permian beds in the Vale of
Eden, while plants occur in the middle division of that series, as men-
tioned by Professor Harkness.
The evidence derived from reptilian remains in the red beds,
so far as it yet goes, is of the same kind as that afforded by the
Keuper sandstones. First we have Dasyceps Bucklandi in the
Permian beds near Kenilworth; next the footprints mentioned
by Professor Harkness in the red sandstones of the Vale of Eden,
as occurring at Brownrigg, in Plumpton, and near Penrith; and
lastly the numerous footprints described by Sir William Jardine,
in the sandstones of Corncockle Moor and other parts of Dumfries-
shire, now universally believed to be of Permian age. All of these
prints indicate that the animals were accustomed to walk on bare
damp surfaces, which were afterwards dried in the sun before the
flooded waters overspread them with new layers of sediment, in a
manner that now takes place during variations of the seasons in
many salt lakes. Pseudomorphs of crystals of salt * in the Permian
beds of the Vale of Eden, and deposits of gypsum and peroxide of
iron, help to this conclusion, together with the occurrence of ripplings,
sun-cracks, and rain-pittings impressed on the beds.
The remaining fossils that require to be considered in the red
sandstones and marls belong exclusively to marine genera.
In Lancashire the Lower Permian red sandstones, which Mr.
Hull estimates as about 1500 feet thick on the banks of the Mersey
and Tame, are unfossiliferous, and the Upper Permian strata, con-
sisting of red marls with bands of magnesian limestone, contain a
few true Magnesian-Limestone species, viz. Gervillia antiqua, Pleuro-
phorus costatus, Schizodus obscurus, S. rotundatus, Turbo helicinus,
T. obtusa, Rissoa Leight, R. Gibson, Natica minima, and some
otherst. They are all small and dwarfed, and in this respect and
the small number of genera they resemble the living molluscan
fauna of the Caspian Sea.
In the true Magnesian-Limestone districts of the east of England
the case is different. There we find a more numerous marine mol-
luscan fauna, but wonderfully restricted when compared with that
of Carboniferous times. From Mr. Etheridge’s unpublished lists it
may be roughly estimated as follows :—
Bracuiopopa. Camarophoria 3, Crania 2, Discina 1, Lingula 2,
Producta 2, Spirifera 3, Spiriferina 2, Strophalosia 4, Terebratula 2:
in all, 9 genera and 21 species.
LameLiisrancniata. Aucellal, Mytilus 2, Avicula 2, Gervilliad,
Arca 2, Cardiomorpha 1, Ctenodontal, Ledal, Myalinal1, Myo-
concha 1, Pleurophorus 1, Edmondial, Astarte 2, Schizodus 5, So-
lemya 4, Tellina 1: in all, 16 genera and 31 species.
Untvatves. Calyptrea 1, Chemnitzia 1, Chiton 3, Chitonellus 4,
* Harkness, Quart. Journ. Geol. Soc. 1862, vol. xviii. p. 215.
t+ Taken from Mr. Hull’s ‘‘ Memoir on the Country around Oldham,” and
eorrected for generic names according to Mr. Etheridge’s lists.
248 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 8,
Dentalium 1, Natica 2, Pleurotomaria 3, Rissoa 1, Straparolus 1,
Turbo 5, Turbonilla 4: in all, 11 genera and 26 species.
Preropopa. Theca 1.
CrpHatopopa. Nautilus 1.
The whole comprises only 38 genera and 80 species.
All of these are small and dwarfed in aspect, when compared with
their Carboniferous congeners, when such there are.
In this poverty and dwarfing of the forms, these Magnesian-Lime-
stone fossils may also be compared with the still less numerous
fauna of the Caspian; and though I am not aware that that inland
sea contains any Corals or Polyzoa, yet I doubt if the presence of
two or three species of Chetetes (3) and Polycelia (2), together with
half a dozen Polyzoa and a very small Cyathocrinus, would entitle
us to assume that it is impossible that they might have lived in an
inland salt lake, which, like the Caspian, had previously been con-
nected with the open ocean.
The Magnesian-Limestone series of the east of England may possi-
bly, however, have been connected directly with an open sea at the
commencement of the deposition of these strata, whatever its subse-
quent history may have been; for the fish of the Marl-slate have
generically strong affinities with those of Carboniferous age, some of
which were undoubtedly truly marine, while others certainly pene-
trated shallow lagoons bordered by peaty flats. But the Marl-slate
fish afford no certain clue to the solution of the problem as to whether
in our area and in other parts of Europe they inhabited open sea or
isolated inland salt waters. Indeed there is much to be said on the
other side of the question from the reptiles found by Messrs. Howse
and Hancock*; for the Lepidotosaurus Duffii, which was found
very near the base of the limestone in marly limestone passing down
into Marl-slate, was a Labyrinthodont Amphibian, and Proterosaurus
Spenert and P. Hua«leyr, from the Marl-slate, were Lacertilian
Reptiles.
Besides the poverty and small size of the Mollusca, the later strata
of the true Magnesian Limestone seem to me to afford strong hints
that they may have been deposited in a great inland salt lake subject
to evaporation. Mr. Sorby, in a paper read before the British
Association in 1856, considers that the Permian dolomite was
chiefly ‘‘ derived from comminuted and decayed calcareous organisms,
and subsequently altered into dolomite,’ and ‘that probably this
alteration was effected by the infiltration of the soluble magne-
sian salts of the sea-water, under conditions not yet clearly ex-
plained, during the period when it became so far concentrated
that rock-salt was frequently deposited, and that the calcareous salt
removed during the change had, by decomposition with the sulphates
of the sea-water given rise to the accumulations of gypsum.”
Gypsum is common in the red marls of the Permian strata and in
* “On anew Labyrinthodont Amphibian from the Magnesian Limestone of
Midderidge, Durham,” and “ On Proterosaurus Speneri and P. Huxleyi from the
Marl-slate of Midderidge, Durham,” by Albany Hancock and Richard Howse
(Quart. Journ. Geol. Soc. 1870, vol. xxvi. pp. 556 & 565).
1871.] RAMSAY—PRETRIASSIC RED ROCKS. 249
other red marls, such as our Keuper beds. Solid dolomite, he goes
on to say, still contains “about one-fifth per cent. of salts soluble in
water, consisting of chlorides of sodium, magnesium, potassium, and
calcium, and sulphate of lime. These, like those in most crystals
formed from solution, must have been produced at the same time
as the dolomite, and caught in some of the solution then present,
which is thus indicated to have been of a briny character.”
There are no solid beds of rock-salt in our Magnesian-Limestone
series, though I see no reason why pseudomorphous crystals may
not occur in the limestones and associated marls.
Mr. Sorby speaks of the Magnesian Limestone as having been
formed in sea-water ; and I presume he means ordinary open sea. I
submit that it may be more probable that all our Permian magnesian
limestone was chiefly or altogether formed in an inland salt lake.
Under such circumstances it appears to me more likely that carbonates
of lime and magnesia might have been deposited simultaneously by
concentration of solutions due to evaporation; for I cannot under-
stand how such deposits could have taken place in an open sea,
where necessarily lime and magnesia only exist in solution in very
small quantities in such a large bulk of water. In the open sea,
indeed, we know of the formation of beds of limestone only by
means of organic agency. ‘The occurrence of gypsum in the marly
strata of the Magnesian-Limestone series helps to this conclusion.
I have also observed in some of the lower strata of the Mag-
nesian Limestone, when weathered, that they consist of a number
of curious thin layers bent into a number of very small convolutions
approximately fitting into each other, like a number of sheets of
paper crumpled together, and conveying the impression that they are
somewhat tufaceous in character, looking almost stalagmitic, as if
the layers, which are unfossiliferous, had been deposited from solu-
tion, and not like ordinary organic calcareous sediment.
In‘an elaborate disquisition on dolomites, in two lectures, Dr. Perey
concludes with the following words :—‘‘ That dolomite has been
formed by the agency of liquids under very ordinary conditions, I
have little doubt will be hereafter fully established by direct and in-
disputable chemical evidence” *. In the ‘ Geology of Canada’ (Logan)
Dr. Sterry Hunt has given the results of his chemical investigations
bearing on geology, in chapters 17-20. At pp. 575-6 he discusses
the subject of dolomites. The passages are too long for quotation ;
but after explaining various natural processes by which he conceives
that mixed carbonates of lime and magnesia may be deposited from
solution in salt water, he concludes that ‘‘these reactions require in-
land seas, or basins cut off from communication with the ocean, while,
on the other hand, the conditions of the production of carbonate of
lime are everywhere found.” The chemical arguments are not what
first led me to suspect that the Permian magnesian limestone was
deposited in an inland salt sea from solution, though I soon after
began to entertain the idea, and to search for evidence on the point.
It is satisfactory to find that eminent chemists take this view with
* Swiney Lectures, 1864, ‘The Chemical News,’ p. 89.
250 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 8,
regard to other dolomites. That the Magnesian Limestone was de-
posited in great part from solutions may partly account for the
absence of fossils in so much of that formation ; and the uncon-
genial nature of the waters of a salt lake may account for the
poverty-stricken character of the whole molluscan fauna.
One other group of red or purple strata remains, older than the
Old Red Sandstone, and of this I speak with more doubt; I mean
the Cambrian rocks. Neither in North Wales nor in the Longmynd
do these rocks afford any indications of life, excepting annelide-
tracks and burrows; for, with some other persons, I consider that
the so-called trilobite Paleopyge Ramsayi is only an accidental
marking simulating the form of a trilobite*. The general absence
of Mollusca in these strata, and the sudden appearance of shells and
trilobites in quantity in the succeeding Zingula-flags, indicates a
sudden change of conditions. There is perfect conformity between
the two formations ; but the change of lithological character is rapid,
and akin to that which marks the change from Upper Silurian rocks
into Old Red Sandstone; only the order of change is reversed.
Believing that the red colour of rocks is apt to be connected with
their deposition in inland waters, I conceive it to be possible that
the absence of marine Mollusca in the Cambrian rocks may be due
fo the same cause that produced their absence in the Old Red Sand-
stone. The presence of sun-cracks and rain-pittings in the Longmynd
beds favours this suggestion. In Pembrokeshire, however, Mr. Hicks
has discovered a Lingulella (L. ferruginea) and Leperditia cambrensis
on two horizons, in strata well down in the purple Cambrian series.
It is, however, worthy of note that the lowest slaty bed in which the
fossil occurs, directly overlies “ olive-green grits and shales” +. These
may possibly mark occasional influxes of the sea into inland waters,
due to oscillations of level. I do not wish, however, to speak positively
on these Pembrokeshire strata. It is nearly thirty years since I
mapped the country, and I should like again to see the rocks in
place before doing any thing more than merely hinting at the subject.
It is worthy of remark, however, that the possible inland origin of
the Cambrian deposits in general is quite consistent with and throws
some light on the statement by Dr. Otto Torell of the occurrence
of land-plants in these strata, supposing this statement to. be
correct.
If I am right in the deductions I have drawn in treating of the
red rocks and magnesian limestone of older date than the Trias,
some remarkable conclusions may be arrived at in connexion with
the inland character of the waters of the epochs to which this and
my previous paper on the New Red Mar! relate.
The old paleozoic area of Bristol and the Mendip Hills and of
adjacent districts nowpartly concealed bysecondary strata stood above
water during the whole of the periods of deposition of the Permian
and Bunter beds, and was not covered with water till these were more
* «The mythical Paleopyge” (Salter, Quart. Journ. Geol. Soc. vol. xxiii.
p. 340).
t Geol. Mag. vol. y. p. 306.
1871.] RAMSAY—PRETRIASSIC RED ROCKS, ~* 251
or less overlaid with the deposits of the Keuper series. The 7’hecodonto-
saurus and Paleosaurus described by Dr. Riley and Mr. Stutchbury
occur in a magnesian conglomerate of Keuperage, which was long con-
sidered to be the equivalent of part of the strata now called Permian.
My explanation of their stratigraphical position is, that these Dino-
saurian reptiles lived upon land moderately elevated all through the
Permian and Bunter epochs, and that subsequently their remains
were buried in the shingly beds of the Keuper inland sea, which
formed the last of a long series of inland continental waters that
prevailed over a large part of the territory now called Europe, from
the close of the Silurian period onward to the Rhetic beds. First,
there are the great lake-formed strata of the Old Red Sandstone ;
secondly, the Carboniferous formations, to a great extent terres-
trial; thirdly, the Permian series; and, fourthly, the Triassic
and partly the Rheetic beds; after which, during Liassic times, by
subsidence, the sea invaded the land, and a mere group of islands
occupied the site of much of what is now Europe. Further, I
think it may be proved that the great continental areas of North
America and Europe, and even of Asia and Africa, were already
sketched out during the long geological period I have indicated, and
that the great similarity in lithological character between the
Permian and Triassic areas of Europe, America, and India is owing
not to any cause producing depositions of red strata from all the
waters of the world at these periods, but simply to special conditions
of inland continentai waters at various epochs of time.
This leads to the important question of the possible continuity of the
same types of terrestrial as distinguished from marine life during the
whole of this long period. Writers on geological subjects have often
been apt to treat of the fossil records of the earth’s history as being
chiefly marine. If, however, the reasoning used in the foregoing
pages 1s good, then we have a series of records indicating continental
land surfaces containing great fresh and salt lakes, extending over a
very large portion of all known geological time; and this, as far as time
is concerned, possesses a significance quite as great as that of the
marine formations, even though some of these inland-formed strata
are almost destitute of the remains of life. Geographical continuity of
continental land during a period that embraces several great geological
epochs implies probable continuity of continental genera, if not of
species. The Labyrinthodontia common to all the formations from
the Upper Trias to the Coal-measure Anthracosaurus bear upon this
point. Thecodont Saurians are both of Triassic and Permian age.
“< Hyperodapedon, Stagonolepis, and Telerpeton,” says Professor Hux-
ley, “ had no stronger affinities with Mesozoic Reptilia than the Pro-
terosauria (Permian), or than some ofthe Labyrinthodonts of the Coal
have with those of the Trias”* ; Telerpeton, he has little doubt, was
altogether terrestrial. Seeing that Hyperodapedon is as nearly
allied to the living lizard Sphenodon as to its Triassic congener Rhyn-
chosaurus, he sees no reason why it may not hereafter be “‘ discovered
in Permian, Carboniferous, or even in older rocks.” With this I
* On AHyperodapedon (Quart. Journ. Geol. Soc, 1869, vol. xxy. p. 149).
252 PROCEEDINGS Of THE GEOLOGICAL SOCIETY. [Mar. 8,
cordially agree. I never could see any sound stratigraphical reason
why the strata in the Elgin country that have yielded Hyperodapedon,
Telerpeton, and Stagonolepis should be separated from the Old Red
Sandstone. The piece of Lias(or Oolite as it used to be called) at
Linksfield, to my mind, does not alter the question. Mr. Geikie, in
a letter lately received, has no doubt that it is a large erratic ice-
borne mass. In Northamptonshire Professor Morris has described a
larger erratic mass of Oolite, 380 yards in length, exposed in a cutting
in Boulder-clay on the Great Northern railway *. I have seen it,
and can vouch for his accuracy. Mr. Judd has since discovered
several such masses of erratic Marlstone, some of them even of
larger size, in the same county, associated with Boulder-clay, and
resting indiscriminately on Oxford Clay, Inferior Oolite, and all
the formations between. These I have also seent. The whole
mass near Elgin, which has been largely quarried, seems to me to
be of the same nature as the great Marlstone and Oolitic erratics
observed by Professor Morris and Mr. Judd. If the Hyperodapedon
of the Trias is nearly allied to a living lizard, it may very well be
equally allied to a lizard of the Old-Red-Sandstone period. In
like manner Teleosaurian Crocodilia go down from our times to
Liassic or even to Permian times. There can surely, then, be no
difficulty in carrying the former two stages lower, to the strata in
which Stagonolepis and Telerpeton occur, and which I still believe
to be true Old Red Sandstone; for, as Professor Huxley has well
remarked, there is no “ necessary relation between the fauna of a
given land and that of the seas on its shores’ +. This applies
to geological time as well as to geographical space.
In conclusion, so vast a continental period as that between the
close of the Silurian and the end of the Triassic epochs must have
witnessed many disturbances of strata, and changes of physical geo-
graphy, though the actual identity of the continent was not ob-
literated thereby. I will only give one comparatively modern instance
to show how a continent may become changed, but still remain the
same continent, notwithstanding great physical alterations involving
upheaval of mountains and the formation of great lakes. From
Upper-Eocene times to the present day it is certain that a great part
of what is now Europe has existed as a continent; and yet the Alps
and the Pyrenees have to a great extent been raised since that
time; and many vast Miocene fresh lakes in various countries,
with a marine interstratification in Switzerland, have been spread
across the plains. These also have disappeared, because their con-
solidated sediments have since been raised in places into mountains.
Finally let me rapidly pass in review what I think we know of
terrestrial as opposed to marine epochs in the British and neigh-
bouring areas of Europe.
* Quart. Journ. Geol. Soc. vol. xix. p. 317.
+ See Brickenden on the Boulder-clay near Elgin (Quart. Journ. Geol. Soc.
1851, p. 291), C. Moore on the so-called Wealden Beds at Linksfield, &c.
(ibid. 1860, p. 445), and A. Geikie on the phenomena of the Glacial Drifts of Scot-
land (extracted from the Transactions of the Geol. Soc. Glasgow, 1863, p. 48).
t On Hyperodapedon (Quart. Journ. Geol. Soc. 1869, vol. xxv. p. 149).
1871.] RAMSAY—PRETRIASSIC RED ROCKS. 253
1. The Cambrian epoch was probably inland and partly fresh
water.
2. The Old Red Sandstone, the Carboniferous series (in great part),
the Permian rocks and Trias (chiefly), were all formed in inland waters
during one long continental epoch. This was by partial submergence
brought to an end during the Liassic and Oolitic epochs, when the
highlands of Britain formed parts of groups of islands along with other
European paleozoic rocks. At the same time true continental land
was never far off; for even in the deposits of the Inferior and Great
Oolites in Lincolnshire and Yorkshire there is evidence of land and
rivers, which land, growing in extent,at length formed by its drainage
the great continental river of the Purbeck and Wealden series, as
shown by the estuarine and freshwater deposits of England and other
parts of Europe. The Dinosauria of this continent had their allies
in older deposits of Permian and Triassic age. The great geogra-
phical areas were the same.
3. A larger submergence closed this terrestrial epoch; and in our
northern European areas the sea attained great width and depth
during the deposition of the Chalk, and all continental continuity of the
old region was entirely broken up.
4. By subsequent elevation of the land above the sea, the fluvio-
marine Eocene strata of Western Europe were formed, including in
the term fluvio-marine freshwater beds of the whole series together
with the London Clay and other formations, all of which were depo-
sited not far from a river-mouth, or at least from shore. With this
latter continent there came in a terrestrial fauna almost entirely
new, and wonderfully different from that which preceded it. From
that day to this, most of Europe has been essentially a continent, and
its terrestrial fauna, in a large sense, of modern type.
If, according to ordinary methods (recognized if not absolutely
true), we were to classify the known old terrestrial faunas (as di-
stinguished from marine) of the greater part of North America,
Kurope, Asia, and probably of Africa, a paleozoic epoch would
extend from the Old-Red-Sandstone at least to Purbeck and
Wealden times, and a Neozoic epoch at least from the beginning of
the Eocene period down to the present day, the Upper Cretaceous
times remaining unclassified; while the marine epochs would be
tolerably correctly, but provisionally, divided also into two,—one,
palzeozoic, embracing the formations from Laurentian (or at least
Silurian) to the close of the Permian times ; and all besides, down to
the present day, would form one great Neozoic or later series. The
terrestrial and the marine series at their edges overlap each other.
In this sense, as regards marine strata, the terms Paleozoic and
Neozoic were first used by Professor Edward Forbes; and the rejec-
tion of the three terms Paleozoic, Mesozoic, and Cainozoic, as applied
to terrestrial faunas, may be inferred from the remarks in Professor
Huxley’s paper on Dicynodon. The great life-gaps between the two
terrestrial series may some day be filled up by the discovery of the
traces of old continents containing fossilized modifications of forms
that accompanied the lapse of time. The generic marine gradations
VOL. XXVII.—PART I. T
254 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 8,
between Paleozoic and later times begin to be discovered even
now.
Note.—After the foregoing paper was written I recollected certain
red Silurian rocks which I had seen in America, known as the
Onondaga Salt-Group, which contain gypsum, salt, and magnesian
limestone. I at once surmised that their origin must have been
similar to that of the red rocks of Britain mentioned in this and my
previous paper on the New Red Marl &c. On referring to Sir
William Logan’s ‘ Geology of Canada’ (1863), I find, p. 346, that he
considers that the gypsum, “hopper-shaped moulds of salt,” and
other signs show that these rocks, part of which are red marl,
“‘ were deposited from waters concentrated by evaporation.”
Professor Dana in his ‘ Manual of Geology’ (1863), p. 249, speaking
of the same strata, says “that the region which in the preceding
period was covered with sea and alive with Corals, Crinoids,
Mollusks, and Trilobites, making the Niagara limestone, had now
become an interior shallow basin, mostly shut off from the ocean,
where the salt waters of the sea, which were spread over the area
at intervals—intervals of days or months it may be,—evaporated,
and deposited their salt over the clayey bottoms,” &c. It is a satis-
faction to find myself so far supported by authorities so eminent,
though neither of them mentions the red colour as a necessary con-
comitant of the inland-water condition of the Onondaga deposits.
Principal Dawson, of Montreal, has also published several papers
in the Journal of this Society, partly illustrative of the Red Rocks
of Nova Scotia. In one of these, “‘ On the Colouring-matter of Red
Sandstones and of Greyish and White Beds associated with them”
(vol. v. p. 25, 1848), he shows that the colouring matter is peroxide
of iron in a fine state of division, and that it is “like a chemical
precipitate,’ and also that the gypsum in these strata is a chemical
deposit : and he considers that these and other phenomena may “ in
some cases serve to distinguish marine from freshwater deposits.”
He does not, however, argue the case precisely on the grounds
advocated in this paper.
Discussion.
Prof. Huxiry was pleased to find that the author, on physical
grounds, extended some views which he himself had, from other
reasons, brought before the Society. He mentioned that there had
lately been found in the fresh waters of Australia a remarkable
fish, which had been considered to be a Ceratodus, but which, in
many characters, was very similar to Dipterus, and in some respects
resembled Phaneropleuron. In other respects it was connected
with Lepidosiren. It was about to be fully described by Dr. Gun-
ther. The fact that this remarkable fish inhabits fresh water,
he thought, corroborated Prof. Ramsay’s argument. He agreed
with the author as to his views respecting the terrestrial fauna
of ancient times, and was quite prepared for the discovery of mam-
malian remains in earlier formations than those in which they are
at present known. He did not so cordially agree with his views as
1871.] RAMSAY—PRETRIASSIC RED ROCKS. 255
to the marine fauna. He would carry back the forms from which
those of the poesent day are immediately derived to Cretaceous
rather than Eocene times. Between the later Cretaceous and the
Permian strata there was a well-defined and characteristic set of
Mesozoic fossils.
Mr. Eruerier commented on the dwarfed condition of our Per-
mian fauna, which corresponds in the main with that of the Con-
tinent, though with fewer genera and species.
Prof. Rupert Jonzs protested against some of the reasons adduced
for regarding some of the areas cited as having been inland lakes,
though no doubt such lakes must have existed. He thought that
mere colour could not be taken as a criterion. If it were, he in-
quired why the bottoms of the present lakes were not red? Many
of the red rocks were, moreover, full of marine fossils. He con-
tended for the true trilobitic character of Palewopyge Ramsayi, and
mentioned its occurrence and that of Lingula ferruginea in red
Cambrian rocks as proving the marine character of the beds. The
Magnesian Limestone he also insisted upon as a purely marine and
open-sea deposit.
Prof. Morris thought the subject required further consideration
before the whole of Prof. Ramsay’s views were accepted. The Cam-
brian beds, for instance, containing great beds of conglomerate,
seemed such as could only be due to marine action, and would
derive their red colour from the decomposition of the old horn-
blendic gneiss from which they were derived. With regard to the
Red Sandstone, he would inquire whether the colour might not be
derived from the decomposition of rocks composed of hornblendic
materials. The Old Red Sandstone beds, though in this country
containing fishes which might be of freshwater genera, had in Russia
the same fishes associated with marine shells; and much the same
was the case in the Trias.
Dr. Carpenter had been led to the conclusion that wherever there
was an inland sea connected with the ocean by a strait even of
moderate depth there was a double current tending to preserve some
degree of similarity between the waters of the two, the difference of
specific gravity in the Mediterranean as compared with the Atlantic
being about as 1:026 to 1:029. In the Red Sea, where so little
fresh water came in, and there was an evaporation of nearly 8 feet
per annum, the water was but little salter than that of the ocean
with which it was connected. In the Baltic there is an under-
current inwards, which still keeps it brackish; but the influx of
fresh water was so enormously in excess of the evaporation, that
‘otherwise it would long ago have become pertectly fresh. Such
facts bore materially on the speculations of the author.
Capt. Spratt maintained that in the Dardanelles there was not a
trace of such an undercurrent as that mentioned by Dr. Carpenter,
In the winter months, when the flow of the rivers into the Black Sea
was for the most part arrested by ice, the salt water of the Medi-
terranean was frequently carried into the inland seas; and these
being much deeper than the channel of the Dardanelles, the salt
T2
256 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 22,
water, by its greater specific gravity, remained in the bottom of the
sea of Marmora, so that, while the upper portion of the water and
that on the shores were diluted to the Black-Sea density, Mediter-
ranean conditions existed in the deep centre of the sea. If, there-
fore, the Black Sea had been pure fresh water, the upper portion of
the Sea of Marmora would have been fresh also, with its fresh-
water fauna, whilst the deeps of that sea would be marine.
Dr. Duncan mentioned that in certain coral reefs intersected by
freshwater currents, the corals still continued to be formed; so that
the existence of dwarfed forms of corals in ancient times was quite
consistent with modern facts.
Mr. Forzes commented on the chemical features of Prof. Ram-
say’s views, and could see no reason why the beds containing iron
should not have been deposited in the open sea. Many beds, for
instance the Gault, contain more iron than those which are now red,
though they may be grey or blue. In sands the grains are often
coloured only superficially with iron, probably derived from sulphates.
In other cases the sands consist of fragments of rocks already red.
There was, in fact, no reason why the beds deposited in the open sea
might not subsequently, by oxidation, become perfectly red.
Prof. Ramsay replied to the remarks of the various speakers, and
summed up by contrasting the usual colour of marine fossiliferous
beds with that of the thick, almost non-fossiliferous rocks of which
he had been treating.
Marcu 22, 1871.
A.R. Selwyn, Esq., Director of the Geological Survey of Canada ;
J. Bridges Lee, Esq., B.A., of Sidney Sussex College, Cambridge,
and 115, Ledbury Road, Westbourne Park, W.; the Rev. Thomas
Robert Willacy, B.A., of Corpus Christi College, Cambridge; and
James Putnam Kimball, Ph.D., of 20 Union Square, New York,
were elected Fellows ot the Society.
The following communications were read :—
1. On the “ Passace-Bups” in the neighbourhood of WooxrHorn,
HEREFORDSHIRE, and on the discovery of a New Spxcrzs of Kuryp-
terus, and some New Lanp-piants in them. By the Rev. P. B.
Broprs, M.A., F.G.S., Vicar of Rowington.
Tue “ Passage-beds” between the Upper Silurian rocks and the Old
Red Sandstone, on the outer area of the Woolhope valley of eleva-
tion, although they have been already noticed by Sir R. Murchison,
Professor Phillips, Strickland, Symonds, and myself, at Hagley,
Tarrington, Ledbury, and Perton have not in this district received
the full attention they deserve ; for although they are of compara-
tively limited vertical thickness when compared with the finer and
more complete sections at Downton and the Ledbury tunnel, they
occupy a larger extent round the valley of Woolhope than has been
previously recognized, and contain some new and interesting fossils
1871.] BRODIE—WOOLHOPE PASSAGE-BEDS. | 257
At Putley, near the road from Ledbury to Woolhope, to the N.E.
of the latter village, a remarkable bed of very hard horizontal
sandstone, composed mainly of small pieces of quartz in a sandy
matrix, overlying a stratum of white and yellow clay, used for
making tiles, may be seen in a brickyard to the depth of about
3 or 4 feet, the blocks of sandstone averaging about 2 feet in thick-
ness. I could find no fossils in it, and it had very much the aspect
of a volcanic rock; but my friend Professor Phillips, to whom I
sent a specimen, recognized it at once, and states that he believes it
to have been derived from Trappean and other Plutonic rocks,
though it may be presumed to be one of the bands of sandstone be-
longing to.this series.. About two miles to the south of Putley, at
a farm called “Chandler’s,” there is a sandstone quarry, which yields
large blocks 13 feet square, having a dip to the north-east, a por-
tion of which is of a very dark colour, almost black, similar to the
peculiar igneous-looking rock just referred to ; and at one place the
strata are much contorted, being thrown up in a small anticlinal.
From the top of Marcle Hill, for at least three quarters of a mile,
in a lane leading to this quarry, on each side of it, there is a thin
band of sandstone, running parallel with the road; but no “olive
shales’ appear above it. Three miles to the north, on Putley com-
mon, near Maine’s wood, other beds of a close-grained more or less
quartzose sandstone occur, in which I found the cast of the larger
form of Lingula cornea. ‘This seems to correspond with the hard
micaceous grit (though there of a purple colour) at the Tin Mills,
Downton, which immediately overlies the ‘olive shales,” and
contains the large Zingula cornea in abundance. The beds were
much disturbed, and more or less inclined, as most of the “ passage-
beds” are here, dipping from the older Silurian rocks of Woolhope,
and in the same direction, for the most part on this side. The par-
tial opening was of no great depth, and therefore the thickness of
the sandstone visible was of limited extent; but judging from the
relative position of the Ludlow formation on the west, and the Old
Red Sandstone on the east, the thickness would perhaps be consi-
derable if fairly exposed. A mile or two towards the north-west,
near Lower Hazle, between this spot and Tarrington, is a small
quarry of thick-bedded variable sandstones, charged as usual with
carbonaceous remains, but finer-grained than those already described.
On the same line, still further towards the north-west, on the brow
of the rising ground called ‘“ Hillfoot,” similar bands of sandstone
are exposed, more or less disturbed, dipping towards the north-
east, and underneath them the “ olive shales,” 3 or 4 feet thick,
passing into, and resting on, a thin stratum of sandstone, similar to
the section at Perton. The shales are horizontal, and contain in the
lower part abundant fragmentary relics of plants, among which are
the seed-vessels of Lycopodiwm, and larger fruits (or sporangia)
which seem to be quite distinct. I could find no Crustacea ; but a
longer and careful search would no doubt detect them. I also
obtained one specimen of the smaller form of Lingula cornea, sup-
posing this species to be identical, which Mr. Symonds thinks it is
258 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 22,
not. In no other places where the: sandstones are present have I
observed these shales, except here and at Perton; but probably,
though not exposed elsewhere, they extend for some distance in this
district, and are to be looked for associated with the sandstones
between the Old Red Sandstone and Upper Ludlow rocks. Owing
tu the very few exposures of rock hereabouts, it is exceedingly diffi-
cult to get any thing like a clear and consecutive section. Here and
at Putley brickyard there is a want of conformity—the only two
places I have noted this ; for, as a general rule, the “ passage-beds”
are conformable to the Upper Silurians. About two miles further
on is the better-known quarry at Tarrington. Six to eight beds of
sandstone, varying in thickness, colour, and lithological character
are exposed here, divided by thin partings of yellow and grey-
coloured clay, having a total thickness of about 20 feet, with a
rapid dip to the north. JI could detect no “olive shales” here; and
tne only fossils are the usual carbonized fragments of plants, including
the characteristic Lycopodites. Some of the blocks of sandstone are of
large size, and no doubt form a useful building-stone. The next expo-
sure of the sandstones, including the “ olive shales,” is at Perton,
which I have already referred to in a short paper published in the
‘Journal’ of this Society *; but as I was unable then to give a de-
tailed section, it may be desirable to add it now in descending order.
ft. in.
1. Divided beds of sandstone in thin bands ..............-.....0% 2 0
2. Dark-coloured brownish shales ............0000csscseeeeecece 3. 0
3° Yelllow sandstone yes sic acter cts ele, otoveh aie ravewategs okt ola) cecvertetcc eastern I G6
4, Olive shales, brown and green, more or less indurated, but gene-
rally very brittle, sandy, and slightly micaceous, and having an
HERA IE MMIC HIN “Conc ob code cu aGodOU hoo Sacdnecoacse spor oc ely)
5, Mhin-bedded| sandstones. ojersl-ns eles ates creisicteieiels l-iclels orien arene 0 5
6. Olive shales, often arenacous, with a thin sandy layer at the base,
similar in structure to No.4 .............. eee ee ee tees 4to5 O
IB tails stains uses oe I ea) AN Ae sd pa 16 11
I was only able to make out this section satisfactorily by the aid of a
ladder. ‘The upper sandstones thin out rapidly to the south-west, the
“ olive shales” rising to the surface, but too high up to be reached.
The lowest stratum (No. 6) crops out at the north-west corner of
the quarry ; and, on the authority of a man who had formerly
worked in it, there is a good, thick, serviceable bed of yellow sand-
stone underneath, though I could see no trace of it. If this should
prove correct, it is probably the Downton sandstone. All the sand-
stones are more or less fossiliferous, and yield the usual remains of
carbonized plants, and abundance of Lycopodites. The Crustacea
appear to be confined to the “ olive shales” (Nos. 4 & 6). Isent up
all I procured to Mr. Woodward ; and he informs me that the greater
number belong to Pierygotus Bankszi, with the exception of a small
tail and three species of Hurypterus, viz. E. pygmeus, E. acuminatus,
and E. abbreviatus. One specimen of this genus consists of a con-
* Quart. Journ. Geol. Soc. vol. xxv. p. 235, March, 1869.
1871.] BRODIE—WOOLHOPE PASSAGE-BEDS. 259
siderable portion of the body ; the others are chiefly fragments of the
body, heads, tails, claws, and swimming-feet. I was fortunate enough
to discover an almost entire specimen of anew species of Hurypterus,
which Mr. Woodward has named #. Brodie, and described at the
meeting of the British Association at Liverpool. He pointed out that
it ‘‘ differed slightly from all other well-known species in the form of
the swimming-feet, in the palpi, but most of all in the form of the
thoracic plate”*. It is perfect from the head to the apex of the
sharp-pointed tail, and measures 23 inches in length, and 10 lines
in the broadest part of the body, and has a portion of one of the
swimming-feet attached”. These shales contain a species of coral
(Actinophyllum), not very common ; but I could observe no shells,
nor the Beyrichie, and only a few of the Leperditic, which charac-
terize them elsewhere.
In addition to the Lycopodites, there are other plants, which I
sent to Mr. Carruthers for determination; he informs me that,
“although very interesting, they are rather fragmentary, and, like
most fossil plants, difficult to determine. The best-marked is a
dichotomously branching plant, which would be referred to an Alga
by most botanists. I believe, however, it is a true land-plant,
which has had vascular tissue in its composition, and a sufficiently
indurated structure to resist decomposition. It may belong
to Dawson’s genus Psilophyton; but more specimens are necessary
before this can be decided. There are several bodies which look
like seeds, but are more probably sporangia. They are certainly
land-plants’’£.
I have not been able to find any traces of the numerous fish dis-
covered at Ledbury and Ludlow ; but it is possible that a closer and
longer search would detect them§. At Prior’s Court, about a mile
south-west of this spot, there is a small exposure of the sandstones,
showing nearly 2 feet of divided beds of yellow sandstone, with car-
bkonaceous remains, resting on the Upper Ludlow, but no “ olive
shales.” At none of these places could I discover the ‘ bone-bed,”
which has been long since noticed at Hagley, not far from this
point on the north-east, first by the late Mr. Scobie, an active
member of the Woolhope Naturalists’ Field Club, and afterwards by
my lamented friend H. E. Strickland, where, many years ago, in
company with the latter and Sir R. Murchison, we found the “ bone-
bed” and numerous remains of Pterygotus; but these were in the
Ludlow rock, and not in the passage-beds which occur there, ac-
cording to my friend Mr. Symonds, who states that they are present
* There are in my collection at least three swimming-feet, and two or more
thoracic plates, of this new species.
t It is imbedded in a yellow, somewhat soft, micaceous sandstone, connected
with the “ olive shales.”
{ It need scarcely be remarked that the occurrence of terrestrial plants,
some of which may very possibly be new, besides those curious bodies long ago
described by Dr. Hooker, and referred by him to Lycopodium, is a matter of
much interest in strata of this age.
§ Mr. Symonds informs me that he has found a P¢eraspis there, which is now.
in the possession of Lord Enniskillen.
260 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 22,
at this quarry. He says that the passage of the Upper Ludlow
rock, with its “‘bone-bed,” may be observed here into the yellow
Downton beds, succeeded by red marls, precisely similar to those in the
Ledbury Tunnel. On my first visit to this spot they were not
exposed, and were not visible at a later one; and the pit has not
been worked now for many years. I cannot, therefore, say decisively
whether the “olive shales” are present there in situ or not. The
“‘ bone-bed” here and at Gamage Ford probably belongs to the
lower “ bone-bed” which, in Shropshire, is present in the higher
portion of the Upper Ludlow, not far below the thicker mass of the
Downton sandstone; while another and upper one occurs about the
middle of the “ olive shales,” but it is apparently wanting here. I
searched in vain for these “ passage-beds ” more to the south, near
Soller’s Hope, where they might be expected to come in, unless a
sandy marl, of which a section may be seen in places along the
brook which traverses the lower ground, belongs to them. It con-
tains a small Orthis and Beyrichia, but it most likely belongs to the
Ludlow formation. They may or may not be continuous round the
whole of the outer limit of the Silurians in the district under review,
and I think it probable that here and there they might be de-
tected in road-side cuttings throughout the whole of this area; I
hope, at some future time, to be able to investigate this more
closely. At any rate, a more considerable extension has been
shown, especially to the east of Woolhope ; and the presence of the
“olive shales,” exactly identical lithologically and, to a certain
extent, zoologically with the “olive shales” near Ludlow and other
places in that neighbourhood, is distinctly proved. On the west,
north-west of Woolhope, and south towards Fownhope, there is less
chance of observing those “ passage-rocks,” if they occur there, be--
cause there is a very considerable quantity of drift, which would
overlie and conceal them. This larger mass of drift, derived mainly
from the denudation of the Silurians adjacent, was first noticed by
my friend the Rev. F. Merewether, Vicar of Woolhope, who, in a
short paper read to the Woolhope Naturalists’ Field Club, in Octo-
ber 1870, has shown a thicker and wider extension of drift in this
direction, which had not been before noticed. In many spots
these ‘olive shales” are not exposed, though they may be present
an situ; but, from their soft and friable nature, a considerable quan-
tity has no doubt been denuded, unless protected by the overlying
sandstones. As they pass downwards into a more sandy stone, it is
probable that there is some sandstone below ; to what extent or
thickness, it is impossible to ascertain ; but it cannot be very thick in
the only two places where I have observed them, as at Perton they rest
almost immediately on the Upper Ludlow, and at Hillfoot, though
not directly overlying it, at least not shown in the section there,
the Ludlow shales crop out not far from them. The subordinate
sandstone would then seem to be of far less thickness than the
more massive sandstone at Downton, Shobden, and elsewhere.
The “ olive shales’”’ are, no doubt, the equivalents in time of the
1871.) WOODWARD—EURYPTERUS BRODIEI. 261
red and blue marls and greenish shales (No. 12) at the ee deLey
tunnel, described by my friend the Rev. W.S. Symonds*, who
remarks that “nowhere else could be seen such a view of the
‘ passage-beds’ between the Silurian and Old Red systems ;” but,
though at no great distance, they are apparently much less de-
veloped along the Woolhope border. I visited this fine section
when the tunnel was being made, with several members of the
Warwickshire Naturalists’ Field Club, and I recollect being much
struck with it at the time. Formerly these “ passage-beds”’ were
classed by Sir R. Murchison with the Old Red Sandstone; but
latterly he has denominated them “ passage-rocks,” which seems alto-
gether more appropriate, as showing their intermediate character
between the Old Red and Silurian. Some geologists, however, I be-
lieve, still desire to have them restored to their original position in the
Old Red. This is a question which I do not pretend to decide,
but which future discoveries of other organic remains may definitely
settle, if it is not already satisfactorily determined, my object being
rather to point out a greater extension of this series around the
~ Woolhope elevation than had been previously recorded.
There are many interesting and important questions connected
with all “‘ passage-beds”’ +, of which several are known to occur be-
tween two great epochs of geological time. It is not impossible that
certain old defined lines of demarcation will ultimately have to be
remodelled or removed, since such transition-periods may be shown
to prove a continuity of the geological record; thus all such “ pas-
sage-beds” may, in fact, be connecting links between one great
geological epoch and another, rather than breaks in the continuity
of succession.
2. On a New Spscies of Evryprervs (EK. Bropier), from Perron,
near Stoke Hpirn, HrrerorpsHire. By Henry Woopwarp,
Ksq., F.G.S., F.Z.8., &e.
In March 1869, the Rey. P. B. Brodie, F.G.S., communicated to the
Geological Society a short account of the occurrence of remains of
Eurypterus and Pterygotus at Perton (see Quart. Journ. Geol. Soe.
xxv. p. 235). Mr. Brodie stated that the specimens collected at
that time and submitted to me were not considered to be new; in
fact they consisted, for the most part, of fragments of Pterygotus t
(P. Banksit) and Eurypterus § (E. pygmeus, E. acuminatus, E. ab-
breviatus, &c.), already noticed by Mr. Salter elsewhere.
Since that communication was read, Mr. Brodie has again ex-
plored this locality, and has forwarded to me several parts and an
almost entire example of a Hurypterus, which differs considerably
* Quart. Journ. Geol. Soc. May, 1860, pt. 2. no. 62.
+ This question was ably treated by Mr, J udd, in a paper lately read at the
Meeting of the British Association in Liverpool.
t{ See Mem. Geol. Surv. Mon. I. 1859, pl. xii. figs. 22-46, p. 51.
§ Quart. Journ. Geol. Soc. 1859, vol. xv. pl. x. p. 229.
262 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 22>
from any species previously examined by me, and of which I beg to
subjoin a short notice.
The most perfect specimen, from which the restored outline (fig. 1)
is taken, measures 22 inches in length, and 10 lines in its widest
thoracic segment. All the somites are united ; and one of the swim-
ming-feet, although injured, is still in place. The head, which is
semicircular in outline, measures 4 lines in length by 9 lines in
breadth ; the eyes are subcen-
tral, and the ocelli nearly cen-
tral, as in the other species of
Eurypterus. The first six seg-
ments (thoracic) succeeding
the head measure together 9
lines in length; commencing
with a breadth of 9 lines, they
increase at the third segment
to 10 lines, and diminish at
the sixth segment to 7 lines in
breadth. The segments in-
crease in length and diminish
in breadth very evenly from
the third segment backwards.
The borders of all the anterior
segments are curved, and the
posterior angles slightly pro-
duced and acutely pointed.
The six posterior (abdo-
minal) segments diminish in
breadth backwards from 6
lines to 2 lines, and increase, Fig. 1. Hurypterus Brodici, H. Woodw.
in the same direction, in length, (outline restored, natural size). Passage-
from 14 line to 24 or nearly beds from the Uppermost Silurian to the
! . Old Red Sandstone, Perton, near Stoke
3 lines, the body being ter- fdith, Herefordshire.
minated by aslender ensiform Fig. 2. Palpus (enlarged).
telson, or tail-spine, 7 lines ¥g. 3. Thoracic plate (enlarged).
in length. No sculpture is
apparent on the segments or head; but the integument com-
posing the former indicates its tenuity by abundance of plice
and wrinkles. The thoracic plate (fig. 3) is very characteristic,
differing in the form of its median appendage from that of any
previously described species. It is 9 lines broad, and 23 in depth;
the median appendage is spindle-shaped in outline, and is 33
lines in length and 13 line broad. The swimming-foot is 24
lines in width, and 2 of an inch in length, exclusive of the basal
joint. The species agrees closely, in the form of its swimming-feet,
with the American and Russian Hurypteri, having the same inter-
calated plate between the ultimate and penultimate joints, and
also the minute terminal palette at the end of the seventh seg-
ment.
Numerous detached endognathary palpi occur associated with this
1871.] WHITAKER—TERTIARY CLIFF-SECTIONS. 263
form, furnished with short recurved spines (fig. 2) arranged in pairs
upon each segment, doubtless referable to the same species. I have
proposed to name this form Zurypterus Brodie, after its dis-
coverer™,
DIscussron.
Mr. Duncan inquired whether any metamorphoses had been re-
cognized among the Eurypteride, and, if so, whether the variation
in the thoracic plates mentioned by Mr. Woodward might be con-
nected with them.
Mr. Woopwarp, in reply, remarked on the difficulty of distinguish-
ing even the sexes in Eurypteride. The thoracic plate in the fossils
resembled that of Zimulus; and the variety might be connected with
sex. In some Slimonie from Lesmahago the only difference to be
found was in the thoracic plate; and it had been suggested that this
was due to difference of sex. He had already suggested that the
small Pterygotus and the great Slimonia might be only the male
and female forms of the same species. On fragmentary remains,
however, it was unsafe to attempt to base species; but he thought
Eurypterus Brodiei was a well-marked species.
Rey. H. H. Wixwoop inquired whether there was any evidence as
to Hurypterus being freshwater or marine.
The Cuarrman (Prof. Morris) observed that the seeds from the pas-
sage-beds did not appear to him other than those of land-plants, and
had been previously described by Dr. Hooker as spore-cases of Lyco-
podiacez.
3. On the Crirr-sxctions of the Tertiary BEDS West of Dieppe in
Normanpy, and at NewHAvEN in Sussex. By Witttam Wuarr-
AKER, B.A. (Lond.), F.G.S., of the Geological Survey of England.
Tue notes from which this paper is made were taken in the summer
of 1866. The two sections described are interesting as showing the
spread of beds that, but for them, would be thought to occur only in
the south-eastern part of the London Basin; and I believe that no
detailed description of the French one has been published, whilst the
English one has been enlarged since the time of its latest descrip-
tion.
1. Dieppe.
The section near Dieppe is noticed by Passyt, in whose time
however, the divisions of the “‘ Lower London Tertiaries” were not
understood, and various superficial deposits were included with them,
the whole being massed under the not very satisfactory name of
< Plastic Clay.”
Mr. Prestwich has referred to this coast in his paper “On the
Woolwich and Reading Series” +; and to him is owing the most im-
* See British Association Reports, Liverpool, 1870, p. 91.
t Descrip. Géol. du Dép. de la Seine Inférieure, 4to: Rouen, 1832.
{ Quart. Journ. Geol. Soc. vol. x. p. 129, 1854.
264 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 22,
portant addition to the geology of the neighbourhood, the mapping
of the London Clay here*, the only part of France, I believe, where
it has been found. :
In the following description the same numbers have been used
for the same beds in the two sections noted, as far as could be.
Westward from Dieppe, along the top of the cliff, there are great
hollows and pipes of Tertiary sand and drift, with many slips, the
clearest giving the section below :—
1. Gravel, of subangular flints and flint-pebbles.
3. Oldhaven Beds? : Fine light-brown, buff, or light-grey sand.
(4. Laminated brown clay.
. | 5. Shelly clay, with a thin layer of shelly stone, over 2 feet.
Light grey (whitish) sharp sand, with ferruginous layers, about a
foot.
2 Grey and brown clayey sand, with peaty layers, especially at bottom,
about a foot.
8. Sharp rather coarse sand, whitish just at top, the rest pale greenish
and yellowish grey, with iron-stains near the bottom. Some small
green-coated fiints, and at the bottom a layer of them (9), 6 or 7
feet, resting evenly on
10. Chalk with flints, but not with such marked layers of them as occur a lit-
tle below.
Woolwich Beds
Further westward the ground falls to the valley of the small river
Scie. Beyond the next gap, which is small, there is at the highest
part a great hollow, of drift loam, flints, and pebbles, and of the
Tertiary beds. All have fallen much, right down to the beach; but
at the top at one spot I saw above the fine sand (3) a mass of clay,
the lowermost part brown and sandy, the rest of a dark greenish grey,
like the bottom London Clay-of East Kent. ‘There may be a fault
here, as the Tertiary beds seem to abut against the Chalk.
At the top of the cliff beyond the next gap, also small, there was
at the time of my visit a very good section reaching for a long way,
and showing the following beds :—
1. Flint-gravel.
Evenly bedded alternations of dark-grey and brown shaly clay,
brown sand (some like that of the Oldhaven Beds), and loam,
Be omen nuk V2jon |p yfeet
ee Brown clayey sand with thin layers of clay, drying hard, 5 or
6 feet ?
3. Oldhaven Beds. Fine light-coloured evenly bedded sand, at one place
with a bed of iron-sandstone more than a foot thick. Over 25 feet.
(The beds below much slipped and not easily to be seen, so that some may
have escaped notice, for instance No. 4. of the former section.)
(5. Shelly clays, much thicker than before, evenly bedded, di-
vided into two by a dark-grey and greenish clay.
A little dark clay with layers of sand.
6.
: Lignite and peaty clay.
Ween A little seey and ferrunots clay.
ees: | 8, Sharp buff sand, with concretionary masses of greywether-
sandstone (as noticed by Mr. Prestwich) and a few flints.
9. Flints in what seems to be a greenish clay (inaccessible) fill-
{ ing small pipes in
10. Chalk.
¥* The Greenough Geol. Map of England, south-eastern sheet, 1865.
1871.] _ WHITAKER—TERTIARY CLIFF-SECTIONS. 265
‘At one place the sand (3) seems to abut against the beds below,
as if from a small fault.
At Varengeville, beyond the next gap, is a like section, the sand
(8) and its included masses of sandstone being in great part white,
and there are also sandy shell-beds. The Oldhaven sand is hidden
by fallen masses from above.
At the next hill the top part of the London Clay contains a bed
of buff sand 2 feet thick.
In Passy’s work a mass of Calcaire Grossier(?) is figured (plate
xix.) as resting unconformably on the beds below. I did not see
it; but it may have fallen into the sea since his time.
Tnland there is a tile-kiln in the London Clay.
2. Newhaven.
The section here was, I believe, at its best when I saw it, the
cliff having been then cut back to the highest ground; and for
this reason I venture to describe it to the Society, although it has
already been described at least five times (three times in the Society’s
publications), and in all these cases by well-known observers, so
that, of course, I shall incorporate their notes with my own.
The shape of the outliers will be seen from the accompanying
map (fig. 1), which differs from that of the Geological Survey in
separating the Tertiary beds into two masses, instead of joining the
whole into one along the face of the cliff. I believe that the mass
Fig. 1.—Geological Map of the Newhaven Outliers.
From Sheet 5 of the Geological Survey Map (1864), with alterations (1866).
Scale 1 inch to a mile.
SS
SS —D
Sata eT Ts
r
© shore
QB
a. London Clay. 6. Woolwich and Reading Beds. c. Chalk. d. Alluvium.
x X Between these points the Chalk is capped by a wash of the Tertiary beds.
of loam, sand, and flints that occurs along the top of the cliff be-
266 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 22,
tween the outliers is not in place, but is reconstructed, being sim-
ply the wash from either side. Another difference is the colouring
as London Clay of a small patch on the more easterly and smaller
outlier, to which alone the following notes refer (the other having
in the cliff nothing higher than the sand of the Woolwich beds ).
Most likely at the time when my friend Mr. Bristow mapped it
(some 12 or 15 years ago) there was no clear evidence of the pre-
sence of this formation, though it was suspected by Mr. Prestwich*.
Fig. 2.— Diagram Section of the Cliff a quarter of a mile west of
Newhaven Harbour.
m
a
etl - = ---- ~~ ---
- -Alluvium.
_ Sea—leveli
a. LondonClay. 6. Woolwichand Reading Beds. ec. Chalk. Gravel omitted.
The dotted lines show the former continuation of the ground and the beds.
Fig. 3.—Section in part of the Western Ditch of Newhaven Fort.
cu
a. Gravel and Sand.
6. Stiff laminated dark grey Clay (Woolwich Beds).
Fig. 4.—Section in part of the Western Ditch of Newhaven Fort.
a, Gravelly Soil. 6. Light-coloured Loam, with gravel at the edge.
e and c’. Stiff brown and grey clay.
Wootich | d. Shelly clay.
; e. Sand, hard and blackish at top, light-coloured below.
The shape of the ground will be understood from the diagram
‘section (fig. 2), which also serves to show how higher and higher
beds have been noticed by later observers. The extent of section
* Quart. Journ, Geol. Soc. vol. x. p. 83.
1871. ] WHITAKER—TERTIARY CLIFF-SECTIONS. 267
described by successive authors is marked by the vertical lines on
the right of the following account, except for the irregular cap of
gravel, which appears in all but the earliest.
1. Coarse red gravel, mostly of subangular flints, but also with flint pebbles,
rather clayey, 10 feet or more.
(Grey and brown clay, sometimes } 10 feet or more,
3 feet. yielding water
5S SPA Fine buff sand, passing into and causing
5 Clay oe 4 Brown and grey loam, passing into } slips.
Basement-bed : flint-pebbles of moderate size in clay
and ferruginous sand, about a foot.
4, Roughly laminated bluish- -grey clay (like London
Clay) about 43 feet (8 feet in Mr. Prestwich’s
section).
(“stot rather hard, clayey, a foot to 2
iB feet or more (5 feet in the earlier account).
Shell 4 st clays, 2 feet or more.
Bede Grey and brown clay, partly sandy, often
with a bed of shells in the middle. 23
feet?
| 5’. Light-coloured sand, partly pink, with thin layers
|
Le bedded grey and brown clay, a few feet.
|
|
of clay and traces of vegetable matter, yielding wa-
ter and causing slips, about 6 feet, passing into
(Grey laminated clay with a few layers of
Prestwich, 1854.*.
Buckland, 1817+, and Mantell, 1822+ and 1833 §.
Wale pil J shells, at one part a thin bed of ironstone
yea Shell with casts of shells, about 8 feet ?
Reading | Beds. | Shelly clay, a few feet.
Soe 4 Clay, with shells at bottom, about 2 feet,
60 feet {below which there is generally
ae | A hard layer, in great part iron-pyrites ? an
pre: inch or more.
ee ee
Webster, 1814),
4 abu dark sand or clay, a few inches.
| te peaty bed. (These three thin beds
| vary ; sometimes the hard layer is absent,
sometimes the lignite.)
7. | grey and brown clay, partly lilac-coloured,
and with large pieces of selenite, 6 feet or more.
8. Light-coloured sand, mostly of a pale yellowish-
; greentint. At one part a bright-red mottled bed
| near the top. In the middle a brown ana appa-
rently harder bed, which projects (not accessible).
9. Bottom bed, green-coated and iron-stained flints
in greensand, about 2 feet. It is from this bed
(or from a local clayey layer at its base) that the
Websterite has come. It rests evenly on
10. Chalk with flints.
The beds seem to vary both in thickness and structure, which
accounts for the slight differences in the various descriptions.
The top of this small but interesting outlier is crowned by a Bri-
x Quart. Journ. Geol. Soc. vol. x. p. 83.
+ Trans. Geol. Soc. (Ser. i.) vol. iv. p. 296.
{ The Fossils of the South Downs, or Illustrations of the Geology of Sussex
(4to, Lond.), p. 257.
§ The Geology of the South-east of England (8yo, Lond.), p. 54. Merely
a shorter reprint of the former as regards this section.
|| Trans. Geol. Soc. (Ser. i.) vol. i1. p. 191.
268 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 22,
tish earthwork, or rather by what remains of it, as about half has
been lost from the gradual wearing backward of the cliff. When
this work was made, the ground must have reached much further
south than now, in the form shown by the dotted line in fig. 2, as
such works are always on hills.
The fort was far from finished when I saw it; but the unfinished
western ditch gave some sections of gravel and loam above and
sometimes wedged into the clays of the Woolwich Beds, as in figs.
3 & 4, which represent part of the same pipe (fig. 3 the western side,
and fig. 4 the eastern).
3. General Remarks.
The Dieppe section seems to show a sort of passage from the
Oldhaven Sand up into the London Clay, layers of sand occurring
in the latter. There is also sand in the same position at New-
haven, where, however, the Oldhaven Beds are not present.
The sections show the extent of the same beds (insignificant as
they are in thickness), or of like conditions, in the Lower London
Tertiaries,—the Oldhaven Sand of Dieppe (3) being just like that of
East Kent*, the shelly clays of the Woolwich Beds both at Dieppe
and Newhaven (5) being the same as those of West Kent (with estua-
rine shells)}, the thin bed of lignite, peaty clay, or firm sand that
occurs throughout Kent occurring also in the sections above de-
scribed (6), and the lowest sand at both (8) seeming to be the same
as that which forms the whole of the Woolwich Beds in East Kent,
and occurs in West Kent also ¢.
The mottled plastic clays are absent ; and the bottom-bed (9) con-
sists of flints partly rolled, as is elsewhere the case where it rests
on the chalk—and not of flint-pebbles, as where it rests on the
Thanet Beds.
Discussron.
The Cuarrman (Prof. Morris), in inviting discussion, called at-
tention to the existence of Tertiary beds of similar character near
Epernay and Rheims, and in other parts of France.
Mr. Evans remarked on the bearing which this extension of soft,
yielding strata had on the excavation of the Channel. The dis-
turbances in the sands and clays might be due to the springs having
formerly, owing to the distarice of the sea and the river-valley not
having been excavated, stood at a higher level, and having thus
softened or washed away the bed beneath the gravels.
Mr. Parrison mentioned that in all the combes along the French
coast towards Tréport there were traces of soft Tertiary beds and
blocks of sandstone.
Mr. WurrakeER, in reply to a question from the Chairman, stated
that, to the best of his belief, the sandstones at Dieppe were not
calciferous. The sands were above the Woolwich beds, and there-
fore not Thanet sands.
* Quart. Journ. Geol. Soc. vol. xxii. p. 410 (bed 3).
+ Mr. Prestwich has given a list of the fossils found at Newhaven.
+ Quart. Journ. Geol. Soc. vol. xxii. p. 409 (bed 2).
Kerk DAWSON—DEVONIAN TREE FERNS. 269
4. On new Tree Ferns and other Fosstus from the Devonian. By
J. W. Dawson, LL.D., F.R.S., F.G.S., Principal of M‘Gill College,
Montreal.
[Puate XII.]
Or the numerous ferns now known in the Middle and Upper Devo-
nian of North America, a great number are small and delicate
species, which were probably herbaceous ; but there are other species
which may have been tree ferns. Little definite information, how-
ever, has, until recently, been obtained with regard to their habit of
growth.
The only species known to me in the Devonian of Europe is the
Caulopteris Peach of Salter, figured in the Quarterly Journal of the
Geological Society for 1858. The original specimen of this I had an
opportunity of seeing in London, through the kindness of Mr. Ethe-
ridge, and have no doubt that it is the stem of a small arborescent
fern, allied to the genus Caulopteris of the Coal-formation. ©
In my paper on the Devonian of Eastern America (Quart. Journ.
Geol. Society, 1862) I mentioned a plant found by Mr. Richard-
son at Perry, as possibly a species of Megaphyton, using that term
to denote those stems of tree ferns which have the leaf-scars in two
vertical series; but the specimen was obscure, and I have not yet
obtained any other.
More recently, in 1869, Prof. Hall placed in my hands an inter-
esting collection from Gilboa, New York, and Madison County, New
York, including two trunks surrounded by aerial roots, which I
have described as Psaronius tevtilis and P. erianus in my ‘ Revision
of the Devonian Flora,’ now in the hands of the Royal Society*.
In the same collection were two very large petioles, Rhachiopteris
gigantea and R. palmata, which I have suggested may have belonged
to tree ferns.
My determination of the species of Psaronius, above mentioned,
has recently been completely confirmed by the discovery on the part
of Mr. Lockwood, of Gilboa, of the upper part of one of these stems,
with its leaf-scars preserved and petioles attached, and also by some
remarkable specimens obtained by Prof. Newberry, of New York,
from the Corniferous Limestone of Ohio, which indicate the exist-
ence there of three species of tree ferns, one of them with aerial roots
similar to those of the Gilboa specimens. The whole of these speci-
mens Dr. Newberry has kindly allowed me to examine, and has per-
mitted me to describe the Gilboa specimen, as connected with those
which I formerly studied in Prof. Hall’s collections. The specimens
from Ohio he has himself named, but allows me to notice them here
by way of comparison with the others. I shall add some notes on
specimens found with the Gilboa ferns, and on a remarkable plant
from the Devonian of Caithness, kindly placed in my hands by Dr.
Wyville Thomson.
It may be further observed that the Gilboa specimens are from
a bed containing erect stumps of tree ferns, in the Chemung group
* Abstract in Proceedings of Royal Society, May 1870.
VOL. XXVII.—PART I. U
270 PROCEEDINGS OF THE GEOLOGICAL society. §[ Mar. 22,
of the Upper Devonian, while those from Ohio are from a marine
limestone, belonging to the lower part of the Middle Devonian.
1. CavLorreRis Lockwoont, n. sp.
(Plate XII. figs. 1 to 3.)
Trunk from two to three inches in diameter, rugose longitudinally.
Leaf-scars broad, rounded above, and radiatingly rugose, with an ©
irregular scar below, arranged spirally in about five ranks; vascular
bundles not distinctly preserved. Petioles slender, much expanded
at the base, dividing at first in a pinnate manner, and afterwards
dichotomously. Ultimate pinne with remains of numerous, appa-
rently narrow pinnules.
This stem is probably the upper part of one or other of the
species of Psaronius found in the same bed (P. ertanus, Dawson,
MS., and P. textilis, Dawson, MS.*). It appears to have been
an erect stem imbedded zn sttw in sandstone, and preserved as a
cast. The stem is small, being only two inches, or a little more, in dia-
meter. Itis coarsely wrinkled longitudinally, and covered with large
leaf-scars (fig. 2) each an inch in diameter, of a horseshoe-shape.
The petioles, five of which remain, separate from these scars with a di-
stinct articulation, except at one point near the base, where probably
a bundle or bundles of vessels passed into the petiole. They retain
their form at the attachment to the stem, but a little distance from
it they are flattened. They are inflated at the base, and somewhat
rapidly diminish in size. ‘The leaf-scars vary in form, and are not
very distinct, but they appear to present a semicircular row of pits
above, largest in the middle. From these there proceed downward
a series of irregular furrows, converging to a second and more ob-
scure semicircle of pits, within or below which is the irregular scar
or break above referred to. The attitude and form of the petioles
will be seen from fig. 1.
The petioles are broken off within a few inches of the stem; but
other fragments found in the same beds appear to show their con-
tinuation, and some remains of their foliage. One specimen
shows a series of processes at the sides, which seem to be the
remains of small pinne, or possibly of spines on the margin of
the petiole. Other fragments show the division of the frond, at
first in a pinnate manner, and subsequently by bifurcation; and
some fragments show remains of pinnules, possibly of fertile pin-
nules. These are very indistinct, but would seem to show that
the plant approached, in the form of its fronds and the arrange-
ment of its fructification, to the Cyclopterids of the subgenus Ane?-
mites, one of which (Aneimites acadica), from the Lower Carbonife-
rous of Nova Scotia, I have elsewhere described as probably a tree
fern}. The fronds were evidently different from those of Archeo-
* Memoir on Devonian Flora, Proceedings of Royal Society, May 1870.
+ Quart. Journ. Geol. Society, 1860.
1871.] DAWSON—DEVONIAN TREE FERNS. 271
pteris *, a genus characteristic of the same beds, but of very different
habit of growth. This accords with the fact that there is in Prof.
Hall’s collection a mass of fronds of Cyclopteris (Archeopteris) Jack-
sont, so arranged as to make it probable that the plant was an her-
baceous fern, producing tufts of fronds on short stems in the ordi-
nary way. The obscurity of the leaf-scars may render it doubtful
whether the plant above described should be placed in the genus
Caulopteris or in Stemmatopteris; but it appears most nearly allied
to the former. The genus is at present of course a provisional one;
but I think it only justice to the diligent and successful labours of
Mr. Lockwood to name this curious and interesting fossil Caulopteris
Lockwood.
I have elsewhere remarked on the fact that trunks, and petioles,
and pinnules of ferns are curiously dissociated in the Devonian
beds—an effect of water-sorting, characteristic of a period in which
the conditions of deposition were so varied. Another example of this
is, that in the sandstones of Gaspé Bay, which have not as yet afforded
any example of fronds of ferns, there are compressed trunks, which
Mr. Lockwood’s specimens allow me at least to conjecture may have
belonged to tree ferns, although none of them are sufficiently perfect
for description.
Mr. Lockwood’s collection includes specimens of Psaronius textilis ;
and in addition to these there are remains of erect stems somewhat
different in character, yet possibly belonging to the higher parts of
the same species of tree fern. One of these is a stem crushed in
such a manner that it does not exhibit its form with any distinct-
ness, but surrounded by smooth cylindrical roots, radiating from
it in bundles, proceeding at first horizontally, and then curving
downward, and sometimes terminating in rounded ends. They re-
semble in form and size the aerial roots of Psaronius erianus ; and I
believe them to be similar roots from a higher part of the stem, and
. some of them young and not prolonged sufficiently far to reach the
ground. This specimen would thus represent the stem of P. erianus
at a higher level than those previously found. My idea of the
possible connexion of these fragments is represented in fig. 3.
Mr. Lockwood’s collections also contain a specimen of the large fern-
petiole which I have named Rhachiopteris punctata. My original
specimen was obtained by Prof. Hall from the same horizon in New
York. That of Mr. Lockwood is of larger size, but retains no re-
mains of the frond. It must have belonged to a species quite di-
stinct from Caulopteris Lockwoodi, but which may, like it, have been
a tree fern.
2. CavLopTERIs antigua, Newberry.
(Plate XII. fig. 4.)
This is a flattened stem, on a slab of limestone, containing Bra-
chiopods, Trilobites, &c. of the Corniferous Limestone. It is about
* The genus to which the well-known Cyclopteris ( Adiantites) hibernicus of
the Devonian of Ireland belongs. :
UZ
272 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 22,
18 inches in length, and 3} inches in average breadth. The exposed
side shows about twenty-two large leaf-scars arranged spirally.
Each leaf, where broken off, has left a rough fracture; and above
this is a semicircular impression of the petiole against the stem,
which, as well as the surface of the bases of the petioles, is longi-
tudinally striated or tuberculated. The structures are not pre-
served, but merely the outer epidermis, as a coaly film. The stem
altogether much resembles Caulopteris Peachi, but is of larger size.
It differs from C. Lockwoodi in the more elongated leaf-bases, and
in the leaves being more remotely placed; but it is evidently of
the same general character with that species.
3. CavLopreris (PROTOPTERIS) PEREGRINA, Newberry.
(Plate XII. fig. 5 and 6.)
This is a much more interesting species than the last, as belong-
ing to a generic or subgeneric form not hitherto recognized below
the Carboniferous, and having its minute structure in part pre-
served.
The specimens are, like the last, on slabs of marine limestone of
the Corniferous formation, and flattened. One represents an upper
portion of the stem with leaf-scars and remains of petioles; another
a lower portion, with aerial roots. The upper part is 3 inches in
diameter, and about a foot in length, and shows thirty leaf-scars, which
are about 2 of an inch wide, and rather less in depth (fig. 5,a). The
upper part presents a distinct rounded and sometimes double mar-
ginal line, sometimes with a slight depression in the middle. The
lower part is irregular, and when most perfect shows seven slender
vascular bundles, passing obliquely downward into the stem. The
more perfect leaf-bases have the structure preserved, and show a
delicate, thin-walled, oval parenchyma, while the vascular bundles
show scalariform vessels with short bars in several rows, in the .
manner of many modern ferns. Some of the scars show traces of
the hippocrepian mark characteristic of Protopteris ; and the arrange-
ment of the vascular bundles at the base of the scars is the same as
in that genus, as are also the general form and arrangement of the
sears. On careful examination, the species is indeed very near to
the typical P. Sternbergu, as figured by Corda and Schimper*.
The genus Protopteris of Sternberg, though the original species
(P. punctata) appears as a Lepidodendron in his earlier plate (pl. 4),
and as a Sigillaria (S. punctata) in Brongniart’s great work, is a
true tree fern; and the structure of one species (P. Cottai) has
been beautifully figured by Corda. The species hitherto described
are from the Carboniferous and Permian.
The second specimen of this species represents a lower part of the
stem (fig. 6). It is 13 inches long and about 4 inches in diameter,
and is covered with a mass of flattened aerial roots lying parallel to
each other, in the manner of the Psaronites of the Coal-formation
and of P. erianus of the Upper Erian or Devonian.
* Corda, Beitrage, pl. 48, copied by Schimper, pl. 52.
1871.] > DAWSON——DEVONIAN TREE FERNS. 273
4. RHACHIOPTERIS, D. Sp.
(Plate XII. fig. 7.)
Along with the above, in Dr. Newberry’s collection, is a singular
fragment enclosed in a large nodule of chert from the Corniferous
Limestone. It shows clearly about 8 inches of the base of an im-
mense petiole, from 4 to 2 inches in breadth, and attached to shreds
of tissue, which seem to represent a part of the stem torn away with
it. Its structure is preserved, and consists of delicate large-celled
parenchyma, with slender bundles of vessels, about eighteen of which
are visible. In structure they are very similar to those of the last
species; but the scalariform vessels are accompanied by more
woody tissue. They are parallel in the distal end of the fragment,
but near its base become tortuous and branching. In the part
which represents the stem, or possibly part of its roots, they as-
sume the form of cylindrical rods of parenchyma with a central
bundle of vessels. In form and outward marking it resembles
R. gigantea of my Royal-Society Memoir; but in the latter the
structure is not preserved. The present specimen must have be-
longed to a tree fern of grander proportions than either of those
previously noticed.
In the cellular tissue of some parts of this great petiole there are
numerous round granules, resembling those figured by Corda in his
description of Protopteris Cottai *, and supposed by that writer to be
grains of fossilized starch. Mr. Carruthers has more recently de-
seribed similar starch-granules in the tissues of an Eocene fernt+.
Whether the granules in the cells of the present specimen are really
remains of starch, or merely rounded siliceous concretions, such as
are often found in the cells of silicified plants, I am by no means
certain. Perhaps the fact that similar round grains are seen in the
interior of some of the woody fibres militates against their organic
character. They are certainly not markings on the cell-walls, but
spherical bodies contained within the cells; and if starch-grains,
they may claim to be the oldest known, being of Middle Devonian
age.
5. Na@e@GERATHIA GILBOENSIS, D. sp.
(Plate XII. fig. 8.)
Leaf rhombic-obovate, with a broad base. Nerves or radiating
plicee nine in number, not forked, and with fine strie between them.
Length 3,2, inches. Breadth 23 inches.
This leaf occurs in the collections of Mr. Lockwood, from Gilboa.
It belongs, without doubt, to the provisional genus Neggarathia,
and seems to have been bent in a conduplicate manner, and clasping
or decurrent, on a stem or branch. It does not seem to have been
a fern; but beyond this I am not inclined to hazard any opinion as
to its affinities.
* Beitrage, pl. 49.
t Quart. Journ. Geol. Soe. Aug. 1870.
274 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 22,
In addition to this species and the Caulopteris above described,
Mr. Lockwood’s collection contains branchlets of a Lepidodendron,
apparently Z. gaspianum, which also occurs in Prof. Newberry’s
collections from the Corniferous Limestone.
6. Lycopopirss, &e.
In his recently published ‘ Paléontologie,’ Schimper (evidently
from inattention to the descriptions and want of access to specimens)
doubts the Lycopodiaceous character of the species of this genus
described in my papers in the Journal of this Society from the
Devonian of America. Of these L. Aichardsont and L. Matthewi
are undoubtedly very near to the modern genus Lycopodium.
L. Vanuxemii is, I admit, more problematical; but Schimper could
scarcely have supposed it to be a fern or a fucoid allied to Caulerpa
had he noticed that both in my species and the allied L. pinneeformis
of Goeppert, which he does not appear to notice, the pinnules are
articulated upon the stem, and leave scars where they have fallen off.
When in Belfast last summer I was much interested at finding in Prof.
Thomson’s collection a specimen from Caithness, which shows a
plant apparently of this kind, with the same long narrow pinne or
leaflets, attached, however, to thicker stems, and rolled up in a
circinate manner. It seems to be a plant in vernation, and the
parts are too much crowded and pressed together to admit of
being figured or accurately described; but I think I can scarcely be
deceived as to its true nature. ‘The circinate arrangement in this
case would favour a relationship to ferns; but some Lycopodiaceous
plants also roll themselves in this way, and so do the branches of
the plants of the genus Ps:lophyton.
In conclusion, I may state that, when in Edinburgh last summer,
Mr. Peach showed me fine and characteristic specimens of rhizomata
of Psilophyton from the Caithness beds, and also specimens which
seem to show that some at least of the fragments from these beds,
which have been referred to Lepidodendron nothum, belong to a
different species, more nearly allied to the Oyclostigma of Killercan
and Gaspé. Mr. Peach has also branches of a Lepidodendron like
L. yaspianum, a Cyclopteris allied to C. Brownii, a plant of the
nature of Anarthrocania or Calanutes, a Stigmaria, and fragments
which may belong to Sigillaria, all from the Devonian beds of
Caithness.
EXPLANATION OF PLATE XII.
Fig. 1. Caulopteris Lockwoodi, one-fourth natural size, portion of stem with
petioles.
Fig. 2. Leaf-scar, natural size.
Fig. 3. Restoration in part of Caulopteris Lockwoodt, reduced: a, upper part,
with petioles; 6, remains of pinne; ¢, middle part, with diverging
aerial roots; d, lower part, with aerial roots, perhaps the same with
Psaronius erianus, Dawson, MS.
Fig. 4. Caulopteris antiqua, Newberry, one-fourth the natural size.
VoL XXVITPUXIT.
Soc
Quart.Journ. Geol.
WIHKGP A)
VWGOIPHgQ
QOH FE Qgg
Sa
Mantern Br o® aap
DEVONIAN TREE FERNS & N@&CCERATHIA.
Wvevalay EGERTON—LIASSIC CHIMMROID FISH. 275
Fig. 5. Protopteris peregrina, Newberry, impression of stem, one-fourth the
natural size: xx, remains of petioles. 54a, scar, natural size, show-
ing bundles of vessels at base ; 54, portion of a vascular bundle, mag-
nified, showing scalariform vessels and cellular tissue; 5c, scalari-
form vessel, highly magnified.
Fig. 6. Lower part of stem of the same, with aerial roots, one fourth the na-
tural size. 64a, one of the roots, natural size.
Fig. 7. Vascular bundle of Rachiopteris, natural size; 7a, portion of the same,
showing vascular and cellular tissue, with rounded granules in the
cells; 76, one of the cells magnified, showing contained granules.
Fig. 8. Neggerathia gilboensis, one-half the natural size.
Discusston.
Dr. Duncan doubted the desirability of basing generic and specific
terms on imperfectly preserved and indistinct specimens, and pointed
out the disagreements among botanists that had resulted from so
doing. He would prefer calling fossils such as those described
“‘eryptogamous forms from certain strata.” He was doubtful also
whether the supposed petrified starch was not merely orbicular
silex.
The Cuarrman (Prof. Morris) remarked on the four different con-
. ditions exhibited by existing tree ferns :—first, with roots running
down the stem; secondly, the lower portion with oval scars; these
are, thirdly, further up the stem, rhomboidal vertically ; and, fourthly,
higher up still, rhomboidal horizontally ; so that were the plant fossil,
distinct genera and species might be founded upon the different parts.
Aprit 5, 1871.
The following communications were read :—
1. On a new Cuimm@ror Fis from the Lias of Lymr Reais (Ischy-
odus orthorhinus, ¢). By Sir Parure Grey Eexrrron, Bart., M.P.,
E.R.S., F.G.S.
[Puare XIII. ]
Txt knowledge we have hitherto obtained of the form and structure
of the fossil fishes assigned to the Chimeroid family is very limited,
being derived solely from the dental plates and dorsal spines, which,
from their superior hardness, have resisted the decomposition
which has removed the more destructible cartilaginous structures
with which they were associated. Whether these old monsters re-
sembled the surviving members of the family in quaint form and
bizarre aspect was a matter of conjecture. That they exceeded them
in size is a matter of fact. The massive mandibles of Jschyodus
Townshendi of the Portland age, or the enormous premaxillaries of
Edaphodon gigas of the Chalk era, sufficiently testify that the pos-
sessors of such powerful dental machinery must have been-of heroic
276. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
size compared with the surviving types of the family. The recent
discovery of a specimen in the Lias of Lyme Regis, in which a
considerable portion of the anterior structures of a Chimeroid is
preserved, enables me to advance a step in clearing up the mystery
which has hitherto shrouded this subject. It was described to
me as a new species of shark, showing the dorsal spine in situ,
and the upper aud lower jaws. From a rough sketch of the spe-
cimen forwarded with the letter, I was inclined to think, from
the peculiar mode of insertion of the spine, that it might possibly
belong to a Balistes or a Siluroid fish, certainly that it could not be
a shark; but on examining the specimen itself I found the unmis-
takable dental apparatus characteristic of the Chimeeroids, sur-
rounded with shagreen ; and then perceived that what was described
as the upper jaw of a shark could only be a monstrous form of the
singular rostral appendage peculiar to the male sex of the Chi-
meroids of the present time. The dermal integument has fortu-
nately retained its proper position and outline on the frontal and
oral regions, representing a tolerably correct profile of the head.
The forehead is characterized by a remarkable prolongation of the
skin (Pl. XIII. fig. 1a), extending six inches beyond the frontal carti-
lages, and terminating in a hook directed abruptly downwards for
more than one inch. This structure is very similar to the prelabial —
appendage found in the Callorhynchus antarcticus of the present period.
Immediately above this projection, and following the outline of its
upper margin, is seen what I imagine to be the homologue of the
frontal ossicle of the recent male Chimeroids (16). In the latter it
exists as a small incurved bone, terminating in a kind of pad covered
with minute spines ; but in the fossil itis developed into a formidable
rostrum slightly curved at the base, forming a frontal declivity, and
then projecting forwards as far as the extremity of the prelabial
appendage above described. Its-entire length is five inches and a
half, of which the anterior two-thirds are straight. The proximal
extremity is attached to the head by means of a rounded condyle,
which is received in a hollow of the frontal cartilage—an arrange-
ment which allows of a limited amount of motion in the vertical
plane. The underside of the rostrum is thickly beset with tubercles
carrying recurved central spines, not unlike the dermal tubercles oi
some of the recent aude. Similar spine-bearing tubercles, seated
on the upper surface of the nasal prolongation, are opposed to the
former, so that a fragmentary specimen of this portion of the fish
might easily be mistaken for parts of an upper and lower jaw. The
tubercles extend in diminished size and numbers along the entire
under surface of the organ. The upper surface was covered by
coarse-grained shagreen, which probably invested also the sides ;
but it has perished in these parts, and the coarse fibrous structure
of the bone is displayed. About one inch behind the insertion of
the frontal spine the orbit is seen. This is of large size, measuring
one inch in diameter. Two inches behind the orbit, and in close
proximity to the occipital region, the dorsal spine (1c) is situated.
Before, however, entering upon the description of this organ, it will
1871.] EGERTON—LIASSIC CHIMHROID FISH. 277
be necessary to allude shortly to the anatomical characters of the
dorsal fin in the recent spinigerous Chondropterygians. Through the
kind assistance of Dr. Ginther, of the British Museum (whose ex-
tensive knowledge of ichthyology is not surpassed by any living
authority), I have been enabled to examine the structure of the
dorsal fin in the recent Acanthias, Callorhynchus, and Chimera. In
the first-named genus, and also in Cestracion and Centrina, the
dorsal fin is supported by a broad cartilage imbedded in the mus-
cular tissue of the back of the fish. The anterior upper angle of
this cartilage carries the dorsal spine, projecting into the cavity of
the spine itself. The spine has its base planted in the muscular
tissue, and is embraced by a fold of skin at the base of the fin.
The internal portion of the spine is defined by the absence of the
horny covering which characterizes the external parts. This feature
is well seen in some of the large fossil Ichthyodorulites. In con-
sequence of this arrangement the spines of these fishes had a
very limited amount of freedom, probably not more than could
be allowed by the elasticity of the integuments. The case is far
otherwise as regards the dorsal spine of Callorhynchus and Chi-
mera, specimens of both which genera have been ably dissected
for me by Dr. Giinther. Here the broad cartilage which supports
the dorsal fin, and which carries the dorsal spine on its anterior
margin, is external to the muscular tissue, and is enveloped only by
dermal integument. The anterior process forming the core of
the hollow spine has its lower extremity developed into a rounded
articulating surface, which works in a cavity on the upper anterior
edge of a strong cartilaginous plate extending upwards from the
notochordal axis. A perfect joint is thus formed (1d), enabling the
spine to move freely in the vertical plane for nearly one-fourth
of a circle, very much as the mast of a barge is lowered and raised
before and after passing under a bridge. In short the Chimeride
had a jointed dorsal spine, the Spinacidee and Cestraciontide a fixed
one. I am not aware that this fact has been noticed before; it is
one of no small importance in considering the natural affinities of
the Chimeroid fishes. In the fossil under description the arrange-
ment of these parts corresponds in all material points with the
recent Chimeroids. The dorsal spine, however, was a more for-
midable weapon. It measures six inches in length from the joint
to the apex, by three lines in breadth. It is slightly recurved, and
is armed with a single series of uncinate spines pointing upwards
on the proximal, and a double series pointing downwards on the
distal, margins of the spine. The remainder of the surface is orna-
mented with fine tubercles arranged in longitudinal lines, and dimi-
nishing in size from the base of the spine upwards. Both these
and the spines consist of a hard lustrous ganoine, similar in ap-
pearance to that composing the tubercles on the rostrum. The
articulating facet at the junction of the spine with the body is
carried on the base of the cartilaginous core which occupies the
cavity of the spine. It differs slightly from the recent analogue
in being rather concave than convex, the corresponding articulating
278 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
surface, on the other hand, being rather convex than concave.
A portion of the membranous fin is seen attached to the hinder
edge of the spine, and is composed of fine-grained shagreen ; im-
pressions are faintly seen in other parts of the specimen, which
show that the dermal covering in general was of the same cha-
racter. The outline of the mandibular region is fortunately pre-
served, and exhibits a very singular truncated form of lower lip.
The labial and mental angles are right angles, and connected by
a straight line one inch in length; the upper and lower margins
are nearly parallel for a distance of one inch from the mentum ;
so that the area of the anterior mandibular projection was a
square of one inch. The dental apparatus is rather dislocated ; but
the component parts remaining are well preserved. There is an
indistinct impression of the left maxillary plate in its proper posi-
tion ; but its fellow of the right side (1 e) is thrown back below the orbit.
This measures one inch and a quarter in length by three lines in
width, being of slighter proportions than the corresponding denticle
of Ischyodus Egertont, which it most resembles. The premaxillaries
are absent. The mandibular plates (1/) are reversed, but retain their
relative positions. Each measures one inch and a half in length,
and is one inch deep at the symphysis. The dental apparatus cor-
responds in all respects with the characters assigned by me to
Ischyodus, to which genus I refer this specimen ; but as it differs
specifically from those already described, I have selected a name signi-
fying its peculiar deviation from the recent types in the size and
form of the rostral appendage.
This remarkable ‘specimen has been secured for the as collec-
tion of fossil ichthyology in the British Museum.
DESCRIPTION OF PLATE XIII.
Fig. 1. Ischyodus orthorhinus, reduced one-third: a, labial prolongation ;
6, frontal appendages; c, dorsal spine; d, articulation of the dorsal
spine; ¢, maxillary plate; f, mandibular plates.
Fig. 2. Rostral tubercle, magnified.
Fig. 3. Outline of the anterior parts of Callorhynchus antarcticus, reduced one-
half: a, labial prolongation ; 6, frontal appendage ; c, dorsal spine ;
d, articulation of dorsal spine.
Discusston.
Dr. GinrHER commented on the interest of this discovery, as in
no other Sharks is the same articulation of the dorsal spine as that
described in the paper to be found. He inquired whether the
granulated plate supposed to be dorsal might not be a part of the
armature of the lateral line, as in Sturgeons. He thought that the
Chimeeroids would eventually prove to be intermediate between the
Ganoid and Shark types, and that all belonged to one subclass.
Mr. Gwyn Jurrreys inquired what other remains were found with
these fishes such as might represent the food, mollnevan or CiieNiaees
on which they lived.
ip it
:
Quart. Journ. Geol. Soc: VeLXXVIL PL
ORTHOREINU
ISCHYODUS
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 279
Sir P. Eerrron replied that there was no deficiency of pabulum
for any kind of fish in the sea represented by the Lias of Lyme
Regis. He also made some remarks on another somewhat similar
specimen in hisown museum. The plate referred to by Dr. Gunther,
he stated, was symmetrical, and not like the lateral plates on the
Sturgeon, which are unsymmetrical. He therefore thought it dorsal.
2. On the Turt1ary Votcanic Rocks of the Britiso Istanps. By
ARCHIBALD GerKi£, Esq., F.R.S., F.G.8., Director of the Geological
Survey of Scotland, and Professor of Geology in the University of
Kdinburgh.—First Paper.
[Puate XTV.|
In the present communication I propose to offer to the Society the
first of a series of papers descriptive of those latest of the British
volcanic rocks which intersect and overlie our Paleozoic and Second-
ary formations, and which, from fossil evidence, are to be regarded
as of miocene, or at least of older Tertiary, date. Materials for this
purpose have been accumulating with me for some years past. In
bringing forward this first instalment of them, I wish to preface the
subject with some general introductory remarks regarding the place
which the rocks seem to me to hold in British geology, and on the
nomenclature which I shall use in describing them. These remarks
will be followed by a detailed description of the first of a succession
of districts where the characteristic features of the rocks are well
displayed. Other typical districts will be described in future
memoirs.
GENERAL [yrRopuUcTION.
1. Area occupied by the Rocks.
The rocks to which I propose to direct attention cover many
hundreds of square miles in the British Islands. They spread over
the north-east of Antrim, from Belfast to Loch Foyle, forming there
a great plateau or series of plateaux, with an area of fully 1200
square miles and an average thickness of 550 feet. From Ireland the
same rocks are prolonged northwards through the Inner Hebrides.
They form nearly the whole of the islands of Mull, Rum, Eigg,
Canna, and Muck. They cover fully three-fourths of Skye, and
extend even as far as the Shiant Isles. But far beyond our own
area they reappear with all their characteristic features in the Faroe
Islands, and again in the older volcanic tracts of Iceland. In
studying the volcanic phenomena which these rocks present to us,
therefore, we are not occupied with limited or local features, but
with the records of perhaps the most remarkable period in the
history of volcanic action in Europe—records which, in spite of the
230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
vicissitudes of later ages, may still be gleaned at intervals over a
length of nearly 800 miles. Throughout that great space volcanic
activity has long been extinct, yet it remains in full force at the
northern extremity in Iceland ; and we may perhaps speculate upon
the possible continuity of the present Icelandic volcanoes with those
which, in Tertiary times, were in action from the Irish Channel far
into the Arctic Ocean.
Nor is it merely by the vast basaltic plateaux which are left that
the former extent and importance of this Tertiary volcanic activity is
to be judged. From the main chain of the Antrim and Hebridean
basalts there diverge innumerable dykes, which are found traversing
Scotland and the north of England, even as far as the shores of the
North Sea. I have elsewhere* given reasons for regarding these
dykes as contemporaneous with the Tertiary volcanic series of the
north-west, and I shall have much to say regarding them in a sub-
sequent paper. Taken in connexion with the great basaltic plateaux,
they furnish us with evidence of a prolonged period of great volcanic
activity.
2. Nomenclature of the Rocks.
Although the petrography of the voleanic series falls to be
described in detail with reference to the localities where the rocks
are found, some general remarks are here required, more especially
regarding the nomenclature which is to be followed}. For the
purposes of a geologist a purely mineralogical or chemical arrange-
ment of rocks is singularly unserviceable. He requires to take cog-
nizance of the geological history as well as of the composition of the
rocks ; and indeed the latter branch of inquiry is chiefly of interest
to him so far as it throws light upon the former. At the same
time he cannot afford to dispense with the aid of chemistry and
mineralogy ; and yet this has only been too frequently the case in
this country, where the nomenclature of our igneous rocks remains
in much the same state as that in which it was half a century ago.
In the course of the researches which are to be described in this
paper, I have found it of great service to keep always prominently
in view the fundamental geological subdivision of volcanic rocks into
Interbedded or Contemporaneous, and Intrusive or Subsequent. Hach
of these two series indicates a distinct variety of volcanic action, the
* Proc. Roy. Soc. Edin. vol. vi. p. 74; Brit. Assoc. Rep. 1867, Address to
Geological Section, p. 52.
+ The word “trap” or “trappean” has been commonly used in this country
as a general term for all these rocks. It has been employed, however, in such
various significations that perhaps it had better be discarded as ambiguous,
unless we agree to use it solely as a convenient synonym for all truly vol-
canic rocks which are found in our Palozoic, Secondary, or Tertiary forma-
tions. As all the rocks which I shall have occasion to describe in this series
of papers are of volcanic origin—either thrown out at the surface in the form of
melted lava, or as loose dust and stones, or injected into different parts of the
rocks lying beneath the surface,—I shall employ the word “volcanic;” only
premising that if at any time, to avoid unmelodious repetition, the word “ trap”
is used, it is to be taken in the sense above indicated. :
1871.) GEIKIE—TERTIARY VOLCANIC ROCKS. 281
former bringing before us the results of that action as shown at the
surface, the latter revealing to us, as no modern volcano can do,
some of those features of the action which go on below ground. It
will be found, moreover, that between the rocks of each series there
is, on the whole, a well-marked petrographical difference. The
same species of rock is sometimes found indifferently in either
division; but when this occurs, as in the case of the dolerites and
basalts, we often learn by practice to discover many little points of
distinction, which, when combined, serve to give us a tolerably
distinctive type for each of the two great series.
In both of these two leading divisions the rocks occur either as
Crystalline or Fragmental. In the former section are included all
the rocks which, like lavas, have been ejected in a melted state; in
the latter those which have been thrown out, like ashes and scorie,
in a fragmentary form.
The Crystalline Interbedded Rocks occur in the form of sheets or
flows, either singly or in consecutive series; they are, in short, old
lava-flows, and present the same general structural and textural
varieties as modern lavas show.
The Fragmental Interbedded Rocks likewise occur in sheets, or
beds or layers; they are the consolidated tuffs, conglomerates, and
breccias arising from the ejection and deposition of ancient volcanic
ashes and scorie.
In the case of the Crystalline Intrusive Rocks I have found the
simplest classification to be one based upon the form of the space
into which these rocks were intruded and in which they consolidated.
Accordingly, I have classed them as 1. Amorphous masses, which
have been thrust through irregular fractures, and show in conse-
quence no parallel bounding surfaces; the syenites of Skye and
Raasay are good examples. . 2. Sheets, which were thrust between
the bedding-planes of older rocks, and which differ from the sheets
of the Contemporaneous Crystalline section in altering the beds
above them, in showing none of the characteristic slaggy upper and
under surfaces found in the contemporaneous flows, and in having
some well-marked lithological differences, such as absence of amyg-
daloidal texture and greater compactness of grain towards the line
of contact with the bounding surfaces of other rocks. 3. Dykes and
Veins. These have resulted from the injection of melted rock along
fissures. When the fissure was more or less vertical and straight,
the intruded melted rock formed a Dyke; when the crack was on a
smaller scale and ran irregularly or branched, either vertically, hori-
zontally, or at any angle, the result was a Vein or series of Veins,
4, In some cases. the original orifices remain, which served as the
vents by which the volcanic rocks were erupted to the surface.
These volcanic pipes are now filled with various kinds of volcanic
materials, and are termed Necks.
The Fragmental Intrusive Rocks only occur as Necks or as Veins
connected with necks. They consist of agglomerate and tuff, some-
times exceedingly coarse and unstratified, composed of fragments of
crystalline volcanic rocks, older tuffs, or of the surrounding strata
through which the neck has been blown out. -
282 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr 5,
This general geological classification admits of and requires further
subdivisions, according to the petrographical distinctions of the
rocks. Thus the Tertiary volcanic rocks which occur as crystalline
interbedded sheets may be grouped, according to their mineralogical
composition, as Felspathic or Augitic. In the former group may be
included the pitchstones, trachytes, and porphyrites; in the latter
the dolerites, anamesites, and basalts. The fragmental interbedded
rocks occur as basalt-tuffs or basalt-breccias. The crystalline intru-
sive series is represented by syenites, quartz-porphyries, pitchstones,
felstones, dolerites, anamesites, and basalts. The fragmental intru-
sive series 1s shown by necks of basalt-agglomerate.
The dolerites, anamesites, and basalts form the great mass of the
Tertiary volcanic rocks of Britain. They occur in vast plateaux, as
in Antrim and the Inner Hebrides, also abundantly as dykes, veins,
and intrusive sheets. They vary in texture from a coarse crystalline
aggregate to fine black basalt, which, in turn, shades into the glassy
variety known as tachylite. In interbedded sheets they are columnar
or jointed, often amygdaloidal, and then full of zeolites. Closely
related to these, and possibly a metamorphosed variety of them, are
some rocks in which diallage occurs in place of augite*. Much less
abundant are some pale grey rocks, sometimes amygdaloidal, occa-
sionally very porphyritic, composed of a dull plagioclase base, with
striated felspar crystals, and for which porphyrite is perhaps the most
fitting name. They occur in interbedded sheets in Mull and Eigg.
Of the more highly silicated igneous rocks, pitchstone occurs some-
what rarely, and always in the form of veins, except in the old
coulée of the Scur of Eigg, to be described in this paper. Felstone
and quartziferous porphyry occur in veins and intruded masses.
Syenite is found in veins, and also as huge hills disrupting and over-
lying liassic rocks in Skye and Raasay. That this syenite belongs
to the Tertiary igneous rocks, and may be connected with the vol-
canic eruptions of the great basalt-plateaux, I hope to show in a
future paper. A rock which has been called a trachyte-porphyry
occurs in Antrim. I may add that around the syenite-hills of Skye,
and possibly also in Mull, there has been developed a local but well-
marked metamorphism of the surrounding rocks +.
The tuffs are comparatively small in quantity. They occur as
thin lenticular layers between the sheets of dolerite forming the
great plateaux, and sometimes, as at Ardtun Head, Mull, and in
Antrim, contain recognizable remains of land-plants. In Mull also
they are sometimes associated with local beds of black cherry-coal,
not distinguishable by any external character from the ordinary
fuel of our coal-fields. Necks of agglomerate are of still rarer
occurrence. Between the sheets of dolerite thin irregular layers of
* These are seen to the south-east of Ben More, in Mull, and seemed to me to
be a continuation of beds which, further west, were ordinary dolerites. In that
area also masses of syenite occur ; and the impression conveyed by a hasty exami-
nation of it was that the volcanic rocks had there undergone subsequent meta-
morphism, as has happened to the Lias limestones round the Tertiary syenite of
Skye. But I propose soon to revisit this interesting district.
+ See Quart. Journ. Geol. Soc. vol. xiv. p. 12 ef seq.
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 283
red bole or earth not unfrequently occur. I have noticed similar
partings between old lavas at Torre del Annunziata; and in the
latter case, at least, they can hardly be regarded as other than the
soil which had gathered over the older lava, and was burnt by the
overflow of the newer one.
The following tabular arrangement will show at a glance the
classification of the rocks which I have adopted :—
Olassification of the Tertiary Igneous Rocks of Britain.
Felspathic Series. B a ponenie oy
yry.
Trachyte and tra-
altered dolerite?
chyte-porphyry.
| Felspathic tuffs.
Felstone and
quartz-porph
| Pitchstone.
| Porphyrite.
| Dolerite.
| Diallage-rock,
Pyroxenic tuffs and
agglomerate.
Basalt.
| Tachylite.
| Syenite.
I. INTERBEDDED OR ConTEMPORA-
NEOUS.
A. Crystalline.
Sheets or beds ......... be leieste 2 |xlelix}*l..| x*
B. Fragmental.
Beds or layers ............ dol)ioo ll ac lealleolledtooheall or {ites
II. Intrusive or SUBSEQUENT.
A. Crystalline.
a. Amorphous masses ...... 3?
MSSBS COS y oicce st ctedaieicis lore +5018 sell eta2 eevee ler ts
y. Dykes and veins ........ x| « | P lx].
Os INGE.) Go bc bcp00macopoo Soi} its
2 ERoes GH
*
2%
IN CCKS ia otictatoiake attic: Sips Sheol sil aaveiel Wee at ated Revi | raya ict pl el level eel | na
In this Table are inserted only those rocks which I have myself,
up to this date, found among the Tertiary series. The list will, no
doubt, be enlarged as further investigations proceed ry.
3. Geological Age of the Rocks.
A few words are needed here in support of the view that all the
rocks now to be described are of Tertiary age. In Antrim the well-
known position of the basalt above the chalk, and its association
with layers containing miocene plants—in Mull the occurrence of a
thick bed of chalk-flints, and of the Ardtun miocene leaf-beds t, at the
base of the whole volcanic series, the evident prolongation of the
Mull volcanic rocks through the other islands of the Inner Hebrides§,
+ I have given a more detailed account of this classification of volcanic rocks,
and of the grounds on which it is based, in Chapter xiii. of the forthcoming
edition of Jukes’s ‘Manual of Geology.’
£ See Quart. Journ. Geol. Soe. vol.vii. p. 90.
§ Following Edward Forbes, I formerly regarded the volcanic rocks of Skye
as of Oolitic age, being misled by the way in which the basalts at their base seem
284 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5,
the passage of the great system of divergent dykes across faults of
every age and through the different geological formations up to and
including the chalk—these are facts which make it sufficiently
evident that in the north-western part of the British area, along the
great hollow stretching from Ireland northwards between the chain
of the Outer Hebrides and the Scottish mainland, volcanic action
was abundantly manifested in miocene times. Whether the erup-
tions took place wholly within the miocene period, or whether they
extended beyond it, into later ages, remains yet uncertain. That
the time during which the eruptions continued was of enormous
duration, is shown by several considerations :—(1) The plateaux are
made up of many successive sheets, each of which marks at least
one, and sometimes more separate eruptions. In Antrim these
sheets rise one over another for a thickness of sometimes 900 feet ;
and how much thicker they may have been cannot now be deter-
mined, seeing that the upper part of the series has been removed by
denudation. In Mull there is a visible thickness of more than
3000 feet of volcanic beds; yet there, too, the upward continuation
of them has been worn away, and there are now no means of mea-
suring what the original total thickness may have been. (2) There
occur among the basalts intercalated layers of tuff, clay, and coal, indi-
cating pauses between the eruptions of long enough duration for the
growth and accumulation of vegetable matter sufficient, when com-
pressed, to form two or three feet of coal*. The leaf-beds of Mull
likewise indicate long and tranquil intervals between the outflow of
successive sheets of basalt. (3) But the most striking evidence of
the long continuance of this volcanic period is furnished in the island
of Kigg, by the occurrence of ancient hollows worn by river-action
out of the basalt plateaux, and subsequently filled by the outpouring
of fresh lava. The latter bears thus the same relation to the more
ancient eruptions that the later coulées of Auvergne do to the old
denuded basaltic plateaux of that region.
But not only have the last-erupted rocks been worn away, and all
evidence removed as to the time when volcanic action ceased to
manifest itself in our area; denudation has since then been so con-
stant and so potent, that even of the whole mass of erupted matter
only disconnected fragments remain. Out of the great basaltic
tablelands long and wide valleys have been carved to a depth of
regularly intercalated with the oolitic strata. As pointed out in a subsequent
page, I have now learned, however, after continued surveys of the other islands,
that this intercalation is deceptive, and that the basalts of Skye are only a pro-
longation of the miocene basalts of Mull.
* Such beds of coal occur in Mull (see Proc. Roy. Soc. Edin. vol. vi. p. 72).
All the coal associated with the volcanic rocks of the Inner Hebrides is of con-
temporaneous, that is of miocene, date. ‘The so-called oolitic coal of Skye I
have now no doubt is of this age; and hence the intercalated strata shown to
occur in the volcanic series of Skye on the map of Scotland published by Sir
Roderick Murchison and myself, and meant to indicate the strips of coal and
associated strata, must be regarded not as oolitic, but as miocene. Their size was
necessarily greatly exaggerated, with the view of expressing the bedded character
of the igneous rocks.
1871.| GEIKIE—TERTIARY VOLCANIC ROCKS. 285
more than 1000 feet. Some of the noblest hills of the Inner
Hebrides are but solitary outliers left standing amid the ruin of the
great sheets of solid rock of which they once formed a part. Ben
More, in Mull, though more than 3000 feet high, is only a mag-
nificent fragment of the huge pile of volcanic material which for-
merly swept over what are now the deep glens and fjords of Mull.
The long lines of imposing cliff with which the basalt plateaux front
the Atlantic all through these islands, from the Fair Head of Antrim
to the far headlands of Skye, tell everywhere the same tale of vast
and continuous denudation. Great, therefore, as the area is over
which these rocks are now to be traced, it covers but a small part of
its original extent.
These prefatory remarks may suffice to show the general nature
of the subject of which I propose to treat, and I shall now proceed
to describe in some detail a district in which some of the phenomena
are typically displayed. The area which I have selected for this
purpose is the island of Eigg, partly on account of its simplicity of
structure, and partly because it presents to us a more striking picture
of the vast duration of the Tertiary volcanic period in Britain than
any other space of like size with which I am acquainted. My
observations are the result of a survey made by me of the island in
the year 1864. In this excursion I was accompanied by my friend
and former colleague Professor Young, of the University of Glasgow,
who devoted himself to the paleontology of the island. It was our
original intention to combine our observations in a joint memoir.
Circumstances having occurred, however, to delay the proper exami-
nation of the fossils, it has been judged expedient to publish, in the
mean time, my own observations on the volcanic geology of the
island, leaving the oolitic strata and their fossils to form the subject
of a future communication.
THE ISLAND OF BIGG*.
A. Puystcan Fraturres anp GEOLOGICAL STRUCTURE.
In the chain of the Inner Hebrides, broken as it is in outline and
varied in its types of scenery, there is no object more striking than
this island. Though only about five miles long and from a mile and
a half to three miles and a half broad, and nowhere reaching a
height of so much as 1300 feet, this little island, from the singu-
larity of one feature of its surface, forms a conspicuous and familiar
landmark. Viewed in the simplest way, EHigg may be regarded as
consisting of an isolated part of one of the great basaltic plateaux
which, instead of forming a rolling tableland or a chain of hills with
terraced sides, as in Antrim, Mull, and Skye, has been so tilted that,
while it caps a lofty cliff about 1000 feet above the waves at the
* The spelling of the Gaelic names on the map and in this memoir has been
landly revised for me by my friend Mr. Alexander Nicolson, advocate, whose
name will be a sufficient guarantee for their accuracy.
YOL. XXVII.—PART I. x
286 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5>
Fig. 1.—Map of the Island of Exgg.
LOG TITTLE?
SGRLSGHL 444117)
2.
Scale of one, Stalule Mile
Or OF Z
|
ffs
|
i
\ LSI
Je
i
|
4
at
i
P. Pitchstone-porphyry cow/ée of the Scir. R. Outcrop of ancient river-gravel
under pitchstone of Sctr. P. Small veins of pitchstone. 6. Dykes, veins,
and intrusive sheets of basalt-rocks. The short black lines traversing the
map in a N.W.-8.E. direction are basalt dykes. jf. Intrusive quartziferous
porphyry. D. Bedded basalt rocks with occasional tuffs. F. Bedded por-
phyrite.
4, Clay with Ammonites, Belemnites, &e.
-= g | 3. Shales and Limestone bands with Cyprids, Cyclas, Ostrea, ke.
S54 2. Thick white and yellow Sandstones with plants.
On ie Shales and Limestone bands with Cyprids, Cyclas, Mytilus, and teeth
and bones of Reptiles.
Xx X. Loch Beinn Tighe. x. Loch a Bhealaich.
»=»—> General dip of the rocks.
1871.] @EIKIE—TERTIARY VOLCANIC ROCKS. 287
north end, it slopes gently along the 7 fh
length of the island to the south end. AS
In the southern half of the island, cans
however, the ground rises, owing to ie E
the preservation of an upper mass of aes
beds, which denudation has removed z Bs 2
from the northern half of the island. ‘S
=|
On this rising part of the plateau 5
stands the distinguishing feature of
the island, the strange fantastic ridge
of the Sctr of EHigg. Seen from the
north or south, this portion of the
island looks like a long steep hill-
crest, ending in a sharp precipice on
the east. But when we get to the
east side, the precipice is seen to be
the end of a huge mountain-wall,
which rises vertically above the basalt
plateau to a height of more than 350
feet. It will be seen from the ac-
companying map (fig. 1) that this
ridge of the Scir corresponds with
the area occupied by a mass of pitch-
stone, and that while the basaltic
rocks cover the whole of the rest of
the southern half of the island, they
gradually rise towards the north, and
successive beds of the oolitic series
make their appearance until, at the
cliffs of Dunan Thalasgair, the latter
cover the greater part of the surface,
and leave the volcanic rocks as a
mere stripe capping the cliffs.
In the accompanying section (fig. 2)
the general structure of the island is
represented.
6b. Dolerite and basalt d
1-4. Oolitic rocks,
F. Porphyrite bed.
Oolitic series.
Beinn Bhuidh,
f}. Intrusive felstone &e.
pp. Pitchstone veins.
D, Bedded dolerites and basalts.
Fig. 2.—Section of the Geological Structure of the Island of Kigg.
B. LiIverRatvreE oF THE SUBJECT.
Volcanic series.
Several geologists have published
descriptions, more or less detailed, of
the mineralogy and geology of this
interesting island. In the year 1800
Professor Jameson gave a brief ac-
count of the different rocks noticed
by him in Eigg; but he did not at-
tempt any description of its geological
structure, further than to notice that
one variety of rock occurred above or
below another. He was then full
c. Ancient river-gravel.
Scr.
B. Intrusive dolerite and basalt sheets.
P. Pitchstone of Sctr.
Table at page 289.
288 PROCEEDINGS OF THE GHOLOGICAL SOCIETY. [Apr. 5,
of belief in the theories of Werner; and as he had found fossil-shells
in one of the sandstones of the island, he went on to speculate on the
probability that the basalt, which alternated with these sandstones,
would eventually be found to contain fossils*. The most detailed
account of Eigg which has yet appeared, is that published by Dr.
Macculloch in 1819+. He pointed out the clear order of succession
of the rocks shown by the cliff-sections, and noticed some of the
more marked varieties, both among the stratified and the igneous
series. He showed also the relation of the secondary rocks to those
of Skye and the rest of the western islands, and connected the
igneous masses with those of the surrounding regions. Although he
visited the island at least twice, he seems to have contented himself
with the examination of those portions which were easiest of access.
Hence some of the most interesting features of the island escaped
his notice. About twenty years later Mr. Hay Cunningham com-
municated to the Wernerian Society a short but interesting paper
upon the geognosy of Higg. He gave some details as to the petro-
graphy of the igneous rocks, but added nothing to our knowledge of
the geology, his remarks on the origin and position of the igneous
rocks beiug founded on a misconception of the twofold interbedded
and intrusive character of these massest. Hugh Miller, in the course
of a cruise among the Western Islands, spent some time at Higg.
His attention was more particularly directed to the fossil-contents
of the oolitic strata, of which he made a collection, and which he
has to some extent described. He did not add any new facts to the
known geology of the island §.
C. Ooxrrie Serres.
Although the detailed account of the Oolitic rocks of Kigg falls
to be given in a subsequent paper, some brief reference to them
may be inserted here. Measured from the sea-level at Tallam to
the base of the overlying sheets of basalt in the cliff at Dunan
Thalasgair, the stratified rocks attain a thickness of probably not
less than 600 feet; though, owing to the way in which they are
split up by intruded sheets of basalt, and concealed by landslip-
rubbish, their depth cannot be precisely determined. As the general
* Jameson’s ‘ Mineralogy of the Scottish Isles,’ vol. ii. pp. 86-47.
+ Macculloch’s ‘Description of the Western Islands of Scotland,’ vol. i. pp.
507-522.
Hay Cunningham, Mem. Werner. Soe. vol. viii., 1839. This author insists
that the igneous rocks of EHigg, as well as those of Scotland generally, were
erupted and consolidated beneath the surface, there being no proof, according
to him, that any of the basalts ever flowed out as a stream at the surface. With
regard to the Scur of Higg, he says, “it can be confidently asserted that it exists
as a great vein, which has been erupted through the older plutonic rocks ”—a
statement which has generally been accepted, but which, as will be shown in this
paper, is wholly inadequate and incorrect.
§ See his ‘Cruise of the Betsy,’ p. 31 e¢ seg.; ‘Sketch-Book of popular Geo-
logy,’ p. 137. Several foreign geologists and mineralogists have noticed the
rocks of Higg. Necker de Saussure gave a detailed description of the miner-
alogy of the Set (‘ Voyage en Heosse,’ ii. p. 449 ez seq.).
2
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 289
dip of the rocks of the island is from north to south, the Oolitic
series is best seen at the north end, whence its different groups of
strata slope northward, until they finally disappear under the vol-
canic series at the Bay of Laig. The following section shows the
order of succession among these rocks :—
Dolerites, basalts, &c. of the plateau.
(4) Clay, with ammonites, belemnites, &c., seen for a short space on the
beach of the south side of Laig Bay.
(3) Hstuarine shells and limestone with Cyclas, Cyprides, Ostrea, &e.
(2) Thick white and yellow sandstones, in some places abounding with
fragmentary plants, and at other parts strongly calcareous, with
numerous casts of Cyclas, &e.
(1) Estuarine shales and limestones, with fossils similar to those in No.
3, and with reptilian bones.
Base of series not seen.
From the general character of these beds, I am inclined to regard
them as on the same horizon with the estuary beds of Loch Staffin,
and with those which in Raasay come in between the Lias and the
Tertiary volcanic rocks—that is, as belonging to the Lower Oolites.
But this subject will require further consideration when the fossils
have been determined.
D. Voxucanic Serres.
The Oolitic strata of Kigg are overlain by a cake of igneous rocks,
which, though it caps the northern cliffs, dips southward with the
underlying strata, until it reaches the sea at Laig Bay on the west
side, and at Kildonan on the east. North of a line drawn between
these two places the igneous capping has been reduced by denuda-
tion to a mere narrow strip, forming the tableland of Beinn Bhuidh ;
south of the same line, it covers the whole breadth of the island.
Yet, although the general inclination of the igneous and aqueous
rocks is in the same direction, a careful survey of them shows that
the former lie unconformably upon the latter. At the south side
of the Bay of Laig, the basalt-rocks rest upon the clays of group No. 1.
As the former are inclined at a slightly less angle than the latter,
they soon creep over their edges, so as to lie upon the shales and
and limestones No. 2. These continue as far as Dunan Thalasgair ;
but there the basalts, after slowly creeping over their denuded
edges for nearly two miles, overlap them, so as to come upon the
massive sandstones of group No.2. The apparent conformity, there-
fore, of the volcanic rocks with the Oolitic strata of the inner He-
brides, which has led to the belief that the volcanic phenomena
were of Oolitic age, is in reality deceptive. I shall on other occasions
have to point out the varied horizons on which these volcanic
masses rest.
The igneous rocks of Higg may be most conveniently described
under three heads :—
1. The Basalt-plateau, marking the oldest eruptions.
2. Intrusive bosses, sheets, dykes, and veins.
3. The pitchstone cou/ées of the Scur, a relic of the last eruptions.
290 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
1. The Basalt-Plateau.
The cake of volcanic rocks which has been referred to as overlying
the Oolitic strata consists of a succession of beds, varying in thick-
ness individually from a few feet to at least 50 or 60 feet, and
having a united depth of not less than 1100 feet. They consist of
dolerites, anamesites, and basalts, porphyrites, and tuffs or breccias.
That they are the result of the outpouring of volcanic material at the
surface, and not of its intrusion among the other rocks beneath the
surface in other words, that they are interbedded or contempo-
raneous and not intrusive or subsequent masses, is shown by the
internal texture of the crystalline rocks, and by the associated tuffs.
Admirable sections are everywhere obtainable along the line of cliffs
by which the island is almost continuously girdled.
a. Dolerites, Anamesites, and Basalts.
By much the larger part of the beds of the basalt-plateau consists
of basaltic rocks (dolerite, anamesite, or basalt). These varieties of
the same great family of volcanic rocks possess the same characters
in Kigg which they retain throughout the Inner Hebrides and An-
trim. The dolerite usually appears as a crystalline granular mass,
passing on the one hand through anamesite into basalt, and on the
other into a coarse aggregate, which shows on its weathered surfaces
large crystals of augite. It is seldom that the rock becomes so black
and compact as to deserve the name of basalt, except in the dykes
to be afterwards described. Examined microscopically, these rocks
fully bear out the observations of Zirkel on the presence of a non-
crystallized matrix in basalt-rocks*. They occasionally abound in
minute needles of apatite, which, along with the beautifully striated
felspar, form a matted network of crystals, through which olivine,
augite, and titaniferous iron are scattered. In some specimens the
decomposition of the minerals is well illustrated. It may be added
that these rocks very closely resemble, in composition and texture,
the crystalline intrusive augitic rocks in the Scottish Carboniferous
series—so closely, indeed, that no line of separation, so far as I
have yet seen, can be drawn between them.
The bedded arrangement of the basalt-rocks, so characteristic of the
vast miocene volcanic region from Antrim to Iceland, is well seen in
Eigg. Along the cliffs at the north end of Beinn Bhuidh, and again
along the south-western shore, the succession of beds is shown
in noble vertical sections, while all over the southern half of the
island the terraced or step-like hill-sides, formed by the outcrop of
the beds, are everywhere visible. Even from a distance, therefore,
the interbedded nature of these volcanic rocks can be readily deter=
mined. The beds range in thickness from perhaps 20 to 50 or 60
feet. They seem quite continuous when looked at from the sea, as
they band the precipices with parallel stripes of darker and lighter
* See his Mikroskopische Untersuchungen uber die Basaltgesteine. Bonn,
1869.
1871. ] GEIKIE—TERTIARY VOLCANIC ROCKS. 291
brown ; and their continuity is still further indicated by the slender
lines of bright herbage which have taken root along the decaying
upper or under surfaces of the flows. Yet, on closer examination,
we find them not unfrequently to die out, the place of one bed being
taken by another, or even by more than one, in continuation of the
same horizon. This is particularly noticeable along the cliff-line
on the east side of Beinn Bhuidh. There is considerable diversity
in the colour and texture, as well as the structure, of the different
beds. Some of them, in which the rock is more compact and
weathered, are divided by vertical joints, which in some cases in-
crease in number till the rock acquires a rudely columnar structure.
This may be admirably seen along the coast north of the harbour,
where a long line of columnar cliff shows in some places curved and
radiating columns. Other beds are formed of a dark compact amor-
phous mass, usually amygdaloidal, and occasionally very markedly
so. A not infrequent variety occurs in the form of a dull green
amygdaloidal and scoriaceous rock, in which balls of more compact
material are wrapped, as it were, in a softer decomposed base. At
the south end of the island, a peculiar band of rock occurs, in which
the process of weathering reveals a succession of layers, a few inches
thick, formed of nodular pieces of compact blue anamesite or basalt,
with a bright red crust. These layers lie a few inches apart, in a
soft, dirty-green, crumbling, and often highly amygdaloidal rock.
The band in which these features are seen runs as an intercalation,
about 3 or 4 yards thick, among the sheets of hard crystalline
anamesite.
As an illustration of the bedded arrangement of these rocks, and
of the way in which they succeed each other along the same hori-
zontal plane, reference may be made to the accompanying diagram
(fig. 3) of part of the cliff-section north of Kildonan, on the east
side of the island.
Fig. 3. Diagram of interbedded Volcanic Rocks on the east side of
Island of Eigg.
TOW MCT VOM
i (il DYNA ye
INL US Ae CS DEN
on aera Lowe PIN e&
TMM
Pap pao Sow %
—— rae Z
ER INNES iG
a CATA
g. Compact jointed dolerite. jf Dull dirty-green decomposing amydaloidal
dolerite. ¢. Compact crystalline dolerite, more finely jointed than bed g.
d. Pale grey porphyrite. c. Dolerite, which a little further north is formed of
several beds. 6. Columnar dolerite. «a. Oolitic strata.
The tests by which the true interbedded or contemporaneous
character of the flows of the doleritic plateau can be determined are
well exposed in Higg. ist. The upper and under surfaces of the
successive flows have very commonly a rough slaggy character, even
when the central portion is compact and crystalline. In this respect
they perfectly resemble sections of recent lava-streams, such,
for example, as those exposed along the Bay of Naples, around Torre
292 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
del Annunziata. In some cases the slaggy upper part of one bed
and the corresponding lower part of the bed above it seem to pass into
each other, although the general bedded structure of the whole re-
mains very marked at a little distance. Here and there, as at the
north end of Beinn Bhuidh, illustrations are afforded of the elonga-
tion of the cavities along the upper surface, showing the direction
in which the lava was moving before it finally cooled and con-
solidated.
2nd. Some of the beds are coarsely amygdaloidal throughout. In
the kernels are found the usual minerals which result from the de-
composition of basalt-rocks—mesotype, stilbite, cale-spar, amethyst,
chalcedony, quartz-crystals, &e. And it is to be remarked, in Kigg
as elsewhere throughout the Western Islands, that the abundance
of the amygdaloidal minerals is proportioned to the amount of alter-
ation which has been undergone by the general matrix of the rock
in which they he.
3rd. Although the interbedded sheets are sometimes seen to die
out along the line of cliff, they never penetrate or otherwise dis-
turb each other. This feature is one which has not been recognized
by previous writers on the igneous rocks of the Inner Hebrides. It
has been lost sight of among the proofs of intrusion furnished by so
many of the basaltic sheets; and thus the “trap” or “ overlying
rocks” of Skye and the other islands have come to be regarded as
typical examples of intrusive igneous masses, and described and
figured as such in innumerable text-books. Yet no fact is more
absolutely certain than that the vast mass of the basaltie rocks of
these regions consists of interbedded sheets, which flowed out,
one over another, at the surface, and have no intrusive characters.
They are traversed, however, by intrusive sheets and dykes, as will
be pointed out in the sequel.
4th. The occurrence of intercalated tuffs, voleanic breccias, and
layers of burnt soil in Eigg, and of shales with remains of land-
plants and seams of coal in the other islands, completes the proof
that the basaltic beds forming the great plateaux, must be regarded
as of interbedded or contemporaneous origin—that is, sheets which
were poured out as lava above ground, and not injected among older
rocks below.
2. Porphyrite.
Under this term I include a well-marked bed, forming a conspi-
cuous band along the range of cliffs which flank the plateau of
Beinn Bhuidh (see figs. 2 and 3). It lies near the base of the
volcanic series. Owing to the flatness of the beds and to denuda-
tion, it has been uncovered, so as to stretch over most of the bottom
of the hollow between Kildonan and the Bay of Laig. But I did
not find it in the southern half of the island. This rock is of a pale
grey colour. It consists of a finely crystalline felspathic base, through
which a few small plagioclase crystals and grains of titaniferous
iron can be seen with the lens. Hxamined with the microscope by
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 293
transmitted light, it is found to consist of a base of plagioclase
felspar, in minute, somewhat decomposed crystals, with abundant
black grains of titaniferous iron, anda brown, much decayed mineral,
which may be augite. The higher part of the bed, at Dunan Tha-
lasgair is darker in colour, and, when examined microscopically,
has much the character of an anamesite. Indeed the whole rock
might be regarded as a highly felspathic basalt-rock in which the
ferruginous silicates are poorly developed.
This rock is, as a whole, strongly amygdaloidal, the cavities in the
upper part of the bed being sometimes so flattened and elongated as
to impart a kind of fissile texture to the mass. This is more par-
ticularly to be noted at the precipice of Dunan Thalasgair. Through-
out a considerable part of the bed, the calc-spar and zeolites of the
kernels have disappeared, and the rock has resumed its original
vesicular aspect.
y. Tuffs, Breccias, Se.
One feature which distinguishes the Tertiary volcanic series of
Britain from those of earlier geological periods is the comparative
paucity and thinness of the intercalated beds of fragmentary ma-
terials. Among the contemporaneous igneous masses of the Silurian,
Old Red Sandstone, Carboniferous, and Permian periods we find
within our own borders enormous beds of tuff and volcanic breccia or
conglomerate ; but. among the great basalt-plateaux of our north-
western tracts such intercalations are represented by mere thin in-
frequent layers. This appears to be the case at least from the south
of Antrim to the north of Skye—the most important tuffs in that
extended area, so far as I am aware, being those of the cliffs at the
Giant’s Causeway. In EHigg this comparative insignificance of the
fragmental as contrasted with the crystalline or lava-form rocks is
characteristically maintained. Throughout the greater part of the
cliff-sections one bed of dolerite or basalt follows another without
the intervention of any dividing layer of tuff or other deposit. Here
and there, indeed, between the beds, we not unfrequently meet with
a thin irregular seam of red earth, which, when fine, might be
called bole. In the cliff below Dunan Thalasgair, for example,
several of the dolerite-beds are not only covered by this substance,
but seem to pass into it. This may be observed also throughout the
Inner Hebrides, and conspicuously along many parts of the Antrim
coast-line. I have recently observed a precisely similar red parting
between several of the lava-streams which have been laid open by
the sea, and by artificial excavations, between Naples and Pompeii ;
and I may add that it is likewise to be observed between the sheets
of melaphyre interbedded with the lower carboniferous rocks of
Kinghorn, in Fife. In all these cases I regard this red layer as
marking a surface of the igneous rock, decomposed into clay or soil
by exposure, and subsequently heated and altered by the overflow
upon it of the next sheet of molten material.
At the north end of Eigg. along the clifis of Beinn Bhuidh, a bed
of coarse doleritic or basaltic breccia is interstratified with the other
294 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
volcanic rocks of the plateau. It consists of a red gravelly matrix
of dolerite débris, in which are imbedded angular and subangular
fragments of various igneous rocks, sometimes a foot and a half long.
Again, at the south end of the island, opposite the rock called
Dubh Sgeir (Black Skerry), the dolerites contain a breccia which
swells out rapidly from a few inches to 6 or 8 feet in thickness ; it
is a rough nodular bed, varying in colour from a dirty green to a
dull red, and consisting of rude angular and subangular pieces of
various dolerites, but more particularly of that on which it lies, im-
bedded in, or wrapped round by, a greenish more or less crystalline
paste, veined with cale-spar.
2. Intrusive Bosses, Sheets, Dykes, and Veins.
The Oolitic rocks, as well as the basalt-plateau which lies upon
them, are pierced by many intrusive masses of igneous rock. These
are all crystalline rocks, no example of any intrusive fragmental
mass, such as the agglomerate of necks, having yet been noticed.
While in the interbedded series the order of superposition furnishes
us at the same time with the relative age of the volcanic beds, among
the intrusive rocks we have no certain guide to relative antiquity,
save the obvious examples where one rock cuts through another.
Nor is it easy to discover any means of ascertaining how far the in-
trusive masses were coeval with, posterior, or anterior to those of the
plateau. The dykes, indeed, must be newer than the interbedded
rocks already described; for they are found cutting through even
the highest of the sheets of the plateau, as well as the intrusive
sheets near or at the base. There is reason to think that the pitch-
stone-veins are yet more recent. But without attempting any
chronological arrangement, let me here describe the intrusive rocks
of Higg, in accordance with the nomenclature above proposed, as
capable of classification after the character of the mould into which
they have been intruded.
a. Amorphous Masses or Bosses.
Only three amorphous intrusive masses were observed by me in
Eigg ; but they possess considerable interest, inasmuch as they serve
to throw some light upon the age of similar masses in Skye. They
consist of felstone (that is, a supersilicated felspar rock, with a
little free quartz), and thus stand out strongly marked from the sur-
rounding basic basalt-rocks. The largest and most characteristic
forms a range of bold cliff, from 150 to 200 feet high, at the extreme
north end of the island. It appears to have risen approximately
along the bedding of the Oolitic strata, and thus to form of itself a
large rude bed. It consists of a pale grey quartziferous porphyry,
traversed by horizontal and oblique veins of basalt. It is quite
columnar in places ; and as the sea has here and there hollowed out
caves at the base of the cliff, the roofs of these recesses expose the
truncated ends of the columns. This rock closely resembles some of
the finer-grained parts of the quartziferous porphyries of Skye and
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 295
Raasay. On the southern declivity, which shelves away from the
base of the Scur, the interbedded dolerites are traversed with an
irregular band of intrusive rock, which weathers into a succession of
rounded knolls along the slope above the ruined hamlet of Lower
Grulinn. This rock varies considerably in different places. For
the most part it has a grey porphyritic base, resembling that of the
grey porphyry of the Scur; in some places, however, it becomes
darker and heavier, and assumes more the character of a doleritic
rock. Possibly more than one variety of rock may here have been
erupted along the same line. The third intrusive mass of porphyry
is shown on the map a little to the east of Laig farm. It is a com-
pact, yellow, quartziferous rock, resembling some parts of the first-
named mass, and weathering with a platy texture. Its exact rela-
tions cannot be here made out; but it cuts through the basalt-rocks,
and is thus later than they are.
Although the full importance of the intrusive bosses of felstone
and quartziferous porphyry in the Tertiary volcanic series cannot
be properly understood from the structure of Higg’, yet the exam-
ples which occur there are of interest, inasmuch as they are found
associated with and penetrating the basalt-rocks, and thus serve
to indicate the true relations of other masses which have invaded
the Liassic and Oolitic strata of the Inner Hebrides at a distance
from the main mass of the basalt-plateau.
B. Sheets.
Geologists are familiar with the often-quoted illustrations given
by Macculloch of the way in which the trap-rocks of Skye have
been thrust between the planes of the secondary strata, so as to run
for a long way strictly parallel to them, appearing as regularly in-
terstratified beds, and then to break across the strata, thereby re-
vealing their true intrusive character*. I have already remarked
that these features, which are characteristic of a certain horizon in
the volcanic series, have been very commonly transferred to the
whole of that series, which is cited in consequence as a kind of
classical example of the intrusive nature of trap-rocks. In reality,
however, the intrusive sheets are almost wholly confined to the
lower portion of the igneous series, and they are quite subordinate
in number and extent to the great interbedded sheets of the
plateau.
So far as I have yet been able to ascertain, it is only the basalt-
rocks which are ever found counterfeiting the parallelism of the
true flows. The petrographical character of these rocks does not,
then, differ essentially from that which they manifest when they
occur as interbedded sheets. Yet, as a rule, they are more compact
and closer-grained, never slaggy, and seldom amygdaloidal. Al-
though the rock is finely crystalline thoughout, the upper and
lower edges of each sheet are more close-grained than the central
* See in particular plate xvii. of his ‘Western Islands,’ where numerous
illustrations are given from the east coast of Trotternish.
296 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
parts. The abundant vertical joints only rarely assume a prismatic
or rudely columnar arrangement. Hence, though it would often be
difficult or impossible to discriminate the intrusive from the inter-
bedded rock in hand-specimens, the distinctions between them are
well maintained when we have a cliff-section before us. This
similarity and difference become readily intelligible when we regard
the two forms as in reality and originally proceeding from the same
source, their distinction being due to the different conditions under
which they were respectively consolidated ; and we then perceive
why the intrusive sheets should lie chiefly at the base of the inter-
bedded series. The former are portions of the Tertiary lava which,
unable to force their way to the surface, escaped laterally along the
lines of least resistance. The increasing mass of the great over-
lying sheets of the plateau would oppose more and more the rise
of the fluid lava, save from the main volcanic vents. Such por-
tions of the latter as were driven up through cracks would often
meet less resistance in trying to force their way along the bedding-
planes of the secondary strata, or between these strata and the
overlying igneous series, or between the lower beds of that series, than
in breaking through the thick and compact volcanic mass above.
Hence it is that, in nature, the intrusive sheets are in reality
found where we might expect to meet with them. These state-
ments involve, no doubt, only the most elementary knowledge.
Yet the want of a due appreciation of this knowledge, and of its
application in the field, has led to grave misconceptions as to the
age of the volcanic rocks of the Inner Hebrides—misconceptions in
which I have myself fully shared. I am naturally anxious, there-
fore, to point out that, while their intrusive relations have been
fully recognized, the pseudo-interbedded character of the intrusive
sheets at the base of the great basaltic plateaux of our west coast
has been confounded with the true interbedded character of the
sheets forming the plateau above, and that hence the inference
regarding the intercalation of contemporaneous volcanic rocks among
the secondary rocks of the Hebrides is without foundation. There
is no evidence of any truly contemporaneous volcanic rock, so far as
I have yet ascertained, in any of the Liassic or Oolitic rocks of
that region. ‘The basalt-plateau, viewed as one great sheet, rests
alternately on Cambrian, metamorphosed Lower Silurian, Liassic,
Oolitic, and Cretaceous rocks, and unconformably upon them all,
from Antrim to the north of Skye. Here and there, where it hap-
pened to be laid down upon more or less horizontal strata, it shows at
its base intrusive sheets which seem to run parallel with it, as well
as with the secondary strata, between which they have been thrust.
And thus has arisen the apparent gradation of the Oolitic groups of
Skye into an upper volcanic series—a gradation, however, which is
quite deceptive, and which disappears when, after wider examina-
tion, we come to recognize the true intrusive character of the inter-
calated sheets, and the real unconformability of the basalt-pla-
teau alike upon Paleozoic and Secondary formations*.
* The suggestion of Edward Forbes regarding the probable Oolitic date of the
1871.] GEIKIUW—TERTIARY VOLCANIC ROCKS. 297
In Kigg the intrusive sheets at the base of the volcanic series are
much less strikingly exhibited than in Skye, Raasay, and Mull.
Some good sections occur, however, at the northend. In the lowest
group of the Oolitic series, as exposed on the shore and on the low
cliff to the east of Blarmor, there is an abundance of thin sheets of ana-
mesite, which, sometimes coincident with, sometimes traversing the
bedding-planes of the shales and limestones, harden the strata along
the line of contact. At that locality the succession of the rocks is
somewhat.obscured by the effects of some large landslips ; and similar
disturbance extends all along the eastern flanks of Beinn Bhuidh.
In one of the streamlets, coming down from that side of the plateau,
Fig. 4. Section of Interbedded and Intrusive Volcanic Rocks,
on the East Coast of Kiggq.
IE 5 er
UP al Woy 8s )
‘\ ( , \ hi
=
— \ 4, 1
: |
~——
1. Sheet of intrusive basalt. 4 to 6 feet thick.
2. Sheet of fine-grained anamesite, 2 to 4 feet thick.
a. Calcareous pale yellow shelly sandstone (Oolite).
6. Columnar fine-grained anamesite or basalt, traversed by intrusive
sheet (2).
e. Dull amorphous fine-grained anamesite.
d. Pale grey porphyrite.
near the Rudh nan tri Chlach, and which is known as the Ault na
horsta mian, more than twenty intrusive sheets of dolerite, anamesite,
or basalt may be counted among the shales and limestones. They are
sometimes mere thin horizontal veins, not six inches thick ; and they
igneous rocks of Trotternish, in Skye, must’ thus be abandoned (see Quart.
Journ. Geol. Soc. vol. vii. p. 104). I adopted his views in my first examination
of Skye; and my reference of the volcanic rocks of Skye to an Oolitic date must
likewise be set aside (Trans. Roy. Soc. Edin. vol. xxii. p. 648; see also Proc.
Roy. Soe. Edin. vol. vi. p. 72, where this change of view is indicated),
298 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
seldom exceed six or eight feet. But perhaps the best examples are
to be seen along the cliffs to the south of Rudh nan tri Chlach. At
this part of the coast, owing to the southward slope of the surface of
the tableland of Beinn Bhuidh, the greater part of the overlying ba-
salts is absent, and only the porphyrite and the underlying beds
form the capping of the cliffs above the Oolitic rocks. The section
(fig. 4, p. 297) represents the succession of rocks there to be seen,
and shows how the intrusive sheets may be intercalated either
with the Oolitic strata or with the older parts of the doleritic
series.
y. Dykes and Veins,
Another mode of escape to the pent-up molten rock was furnished
by long straight fissures and by irregular winding cracks—the former
giving rise to dykes, and the latter to veins. I reserve for a future
paper a full consideration of that remarkable feature of the Tertiary
volcanic rocks, the long parallel dykes. With regard to those which
occur in Kigg, I may remark that they are not remarkable for
numbers or other peculiarities, but that they exhibit many. of
the characteristic features of the dykes which range from the
basaltic plateaux of the Hebrides across Scotland and the north
of England. They run, as a rule, persistently from north-west
to south-east, varying in breadth from a few feet to a few
yards in breadth. They consist either of a close-grained ana-
mesite or of basalt, and sometimes contain large grains of olivine.
They cut across even the newest of the sheets of the plateau, as
may be seen along the terraced slopes that descend from the Seur.
But in some of the cliff-sections, as, for example, below Bideann
Boidheach and on the east side northwards from Kildonan, they may
be seen rising through the lower, but stopping short of the higher
beds of dolerite. That truncation may not indicate that where it
occurs the dykes are older than the interbedded flows which cover
them, but only that the fissures through which they rose did not
extend further upward, or at least did not receive an injection of
lava into their upper parts. At the same time, there can hardly
be any doubt that the dykes as a whole are contemporaneous with
the eruptions of the plateau, some of them belonging to earlier,
others to later stages in the long volcanic history. No dyke has
been observed cutting the pitchstone of the Scur; but several are
covered unconformably by that rock (see fig. 10).
The igneous veins by which the rocks of Higg are traversed do not
differ in origin from the dykes ; but their smaller size and irregular
form enable us to group them by themselves, and to note among
them some characteristic features which are not found, or at least
found much less distinctly, among the dykes. The veins may be
arranged in two groups, according to their component rock, viz. :—
Ist. Basalt veins; and, 2nd. Pitchstone and Felstone veins. ‘This
classification may be regarded as also a chronological one, since
there is reason to believe that the former group is older than the
latter.
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS, 299
1. Basult, Anamesiteand Dolerite V eins.—Theseare closely connected
both with the dykes and with the intrusive sheets, into either of which
any vein may pass, or from which any vein may proceed. They
commonly consist of a very compact finely crystalline rock, often
paler in colour than that of the interbedded basalt-rocks, even where
these are most close-grained. These features may be well seen
along the coast-sections to the north of Kildonan. Among the veins
of that as well as of other localities, a minutely amygdaloidal tex-
ture is occasionally observable, the small kernels being arranged in
lines parallel with the sides of the vein and most marked along its
centre. The grain of the rock usually becomes very close towards
the edge of the vein, passing sometimes through various stages of
flinty basalt into bright black lustrous tachylite. The most perfect
example which I observed of this difference between the texture of
the central and outer parts of a vein occurred in a vein which tra-
verses the basalts on the east side of the Beinn Tighe—one of the
outlying hills of the Scur ridge. The rock is of a dark, very fine-
grained basalt, which along the walls of the vem assumes a vitreous
aspect, and sends out a loop or thread of black pitchstone-like tachy-
lite into the surrounding interbedded basalt (fig. 5). The marginal
crust of tachylite varies in thick-
ness in different veins, ranging from Fig. 5. Plan of Basalt Veins
one-third to about one-eighth of with Tachylite edges, Kast
an inch. Sometimes it shades into Side of Benn Tighe, Kigg.
the basalt within ; in other cases it
forms a pellicle, which cracks off in
weathering. Itis one of the most
opaque rocks I have ever encoun-
tered ; In several slices of it which
I have had prepared for microscopic
examination and reduced to ex-
treme thinness, I am unable to get
any light sent through, even at the
edges.
The veins run vertically, horizon-
tally, or at any angle, and branch
or unite, swell out or diminish, in
a capricious manner. Their close
texture and abundant joints make
them weather differently from the
rocks which they traverse. This, added to a frequent difference of
colour, renders them a conspicuous figure along the coast-cliffs of Kigg
(see fig. 6). Some striking illustrations occur on the east side of the
island north of Kildonan, and also on the great precipice below
Bideann Boidheach, where the pale thread-like veins may be dis-
tinguished even from a distance as they rise along the sombre face
of the cliffs.
2. Pitchstone and Felstone Veins—Although nearly the whole of
the veins in EKigg are protrusions of doleritic rock, there occur a few
in which the rock is pitchstone and, in one case at least, felstone.
That these veins are, on the whole, later than those just described
300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
may be inferred from the fact that the pitchstone of the Scur, as
will be shown in the sequel, is much
younger than the rocks of the basaltic Fig. 6. Basalt Veins tra-
plateau. The pitchstone of most of the versing interbedded Dole-
veins differs, indeed, microscopically rites, Kildonan, Higg.
from that of the Scir; but the latter
varies greatly even within itself, so that,
though no evidence exists of any pitch-
stone vein having ever been connected
with the rock of the Scur, we may, pro-
visionally at least, class all the pitch-
stones together as the latest of the
igneous rocks of Eigg.
Four separate veins of pitchstone
have been noticed in Kigg. ‘The best-
known and most clearly exposed veins
are two which traverse the dolerite beds
aauil
| HULeH r g
at Rudh an Tangairt, near the famous | | | a
| i)
aa
Uamha Fhraing, or Frank’s Cave, on ae ese |
the south side of the island. The “aK Wp Siggy.
eastern vein (fig. 7) consists, in its upper aren PELE;
part, not of pitchstone, but of a pale compact quartziferous porphyry
or felstone, like that of Scorr Scalleadh*. It is exceedingly hard,
splintering under the hammer fig. 7, Vein of Pitchstone traversin
with a metallic sound. It fF Dolerite, ae an Tangairt. _
weathers with ayellowish or pean
reddish tint, which extends for 7
an inch or two into the stone,
and shows numerous cavities,
resulting apparently from the
decomposition of felspar crys-
tals. Towards the margin of
the vein it assumes a laminar
texture, in plates which are
in a general sense parallel to
the walls of the vein. Exa-
mined in thin section with
the microscope, this rock
shows a curious confused mass
of minute needle-like or hair-
like bodies, with opaque par-
tially decomposed grains of
pyrites, or possibly titaniferous
iron, and a still more decom-
posed brown mineral. The texture closely resembles that of some
of the pitchstones. The vein has a thickness of about 23 feet, and
* An engraving of this vein is given by Jameson in his work already cited,
vol. il. p. 45. The felspathic rock he terms “ hornstone;” it is called “ chert”
by Macculloch, and “porphyritic compact felspar” by Hay Cunningham. It
differs in minute structure from evey other rock with which [I am acquainted,
and, as stated in the text, more nearly resembles pitchstone.
1871.] GEIKIE—TERIJARY VOLCANIC ROCKS. 301
runs across the dolerite beds with a trend from N.10° W. Descending
the upper part of the cliff, the vein continues downward ; but the por-
phyry is replaced by pitchstone, which descends to the beach. A
detached portion of the former rock is involved in the latter; but it
is hardly possible to decide here which is the newer mass, or if they
are not of contemporaneous origin *.
The portion of the vein filled with pitchstone runs with a much
less even course and regular thickness than the part filled with por-
phyry. The pitchstone suggests the idea of intense liquidity, as it
seems to have thrust itself into every minute crevice of the crack in
the dolerites up which it rose. Its path is somewhat tortuous; and
its width varies from a few inches to 2 feet or more. Sometimes its
walls are upright and parallel like those of a dyke; but in a little
distance this feature disappears, and the pitchstone bends now to one
side, now to the other, along the irregularly jointed surface of the
dolerites. At the margin of the vein it is deep jet-black, and as
glassy and lustrous as bottle-glass, but much more brittle ; away from
the edge it assumes the ordinary dull resinous lustre of pitchstone,
while in the middle, where the vein is broadest, the rock takes a
porphyritic texture. Examined microscopically, the outer or jet-
black obsidian-like part of the vein is a perfect glass, of a pale brown
colour, this hue being equally diffused as a tint through the mass,
and not arising from the abundance of coloured crystals. I have not
been able, even with a magnifying power which renders an object one
five-thousandth of an inch in diameter clearly visible, to resolve this
coloured matrix into component crystallites, grains, hairs, or any
other structure. It is traversed by minute cracks, which, along
with elongated cavities, run in one general direction parallel with
the sides of the vein. On either side of these cracks the colour has
in some cases been bleached out of the rock for a short distance ;
in others the colour is intensified into a deep brown. The cavities
vary from one two-thousandth of an inch or less up to one fiftieth of
an inch or more, sometimes empty, sometimes filled with a brown
colouring-matter.
About four yards west from the
Fig. 8. Pitchstone filling a cavity vein just described a second vein
in Dolerite, Higg. of pitchstone is seen traversing the
compact close-grained dolerite or
anamesite of the cliffs. Atthe up-
per part of the cliff a detached
portion (which, however, is pro-
bably only a part of the vein) fills
up a cavity like a pot-hole, about
a foot broad (fig. 8). Itis traversed
by numerous divisional planes,
which run parallel with the sides
of the cavity, and converge towards
its bottom in such a way as to look
* Hay Cunningham found liquid bitumen in cavities of this rock.
VOL. XXVII.—PART I. xe
302 PROCEEDINGS OF THE GEOLOGICAL SOCIBTY. [Apr. 5,
like a mass of rather viscid pitch which had been spilt at the top of
the cliff, and had slowly flowed into and filled a cavity in the rocks.
This detached portion of pitchstone has the same bright deep jet-black
or bluish-black colour and obsidian-like texture noticed in the pre-
vious vein. A little below it the main portion of the vein descends the
lower part of the cliff, and crosses the beach from N. 25° W. to 8S.
25° K., with an average width of 14 to 2 feet. Its external parts, .
as in the previous example, are black and quite glassy ; the central
portion possesses the common dull resinous lustre and dark-green
colour characteristic of pitchstone. A thin section of the latter
part of the vein, placed under the microscope, shows that the base
of the rock is a nearly colourless homogeneous glass, through
which are scattered abundant black or greenish hairs of some ferru-
ginous silicate arranged singly and in oblong tufts. The individual
hairs of each tuft are not feathered, like those of the Corriegills pitch-
stone of Arran. It is to the abundance of these pari that the
dark colour of the rock is due.
A third, less distinctly traceable vein of pitchstone traverses the
dolerites on the beach at the harbour. There is the same difference
of texture in it asin the Rudh an Tangairt veins. ‘The black brittle
obsidian-like portion, when examined microscopically, shows a deep
rich-brown homogeneous glass, with numerous small kernels, some of
which are filled witn an amber-coloured substance (bitumen ?).
Except for its much deeper colour and the presence of coloured
kernels instead of much more minute elongated vesicles, the minute
texture of this rock is analogous to that of the east vein. The dull
dark-green portion is markedly porphyritic, and is mixed up, even
in hand-specimens, with the more glassy variety. Under the micro-
scope it shows considerable opacity, but on extremely thin edges
and in certain less deeply coloured portions is found to consist of a
thickly aggregated mass of minute black hairs, less distinctly sepa-
rated than those of the Rudh an Tangairt vein, and imbedded in a
glass mostly of a dark-green or black colour, but here and there
colourless. The colouring-matter is therefore not entirely depen-
dent in this rock upon the abundance of the hair-like particles.
Large crystals of a beautifully striated felspar are scattered through
the rock, also kernels filled with a brown or amber-coloured sub-
stance, as in the biack part of the vein.
A fourth pitchstone occurs on the roadside, a little to the east of
Laig Farm, and seems to be connected with the intrusive boss of
quartziferous porphyry there. It differs considerably in external
aspect from the other veins, being of a pale-green or greenish-grey
colour, and thus resembling at first sight the pale slag of an iron-
furnace. The base is minutely granular, and shows a few scattered
felspar crystals. Under the microscope this rock appears as a pale-
brown glass, through which are scattered abundant minute cavities,
short dark bodies ‘resembling the “hairs” already described, but
less definitely formed, and erystals of an orthoclase felspar.
Petrographically considered, the pitchstone veins of Kigg present
us with three varieties :—1st, those formed of a colourless glass and
1871.] GEIKIE— TERTIARY VOLCANIC ROCKS. 3038
owing their dark hue to the abundant included hair-like agerega-
tions of a ferruginous silicate; 2nd, those formed of a coloured
glass in which the colouring-matter is impalpably diffused ; and, 3rd,
those formed of a coloured glass where the hue is further intensified
by the abundance of included “ hairs.”
3. Pitchstone and Porphyry Coulées of the Scur.
That feature of the island of Kigg which renders it so remarkable
and conspicuous an object on the west coast is the long ridge of
the Scur. Rising gently from the valley which crosses the island
from Laig Bay to the Harbour, the basaltic plateau ascends south-
westwards in a succession of terraces, until along its upper part it
forms a long crest, from 900 to 1000 feet above the sea, to which it
descends on the other or south-west side, first by a sharp slope, and
then by a range of noble precipices. Along the watershed of this
crest runs, in a graceful double curve, the abrupt ridge of the Scur,
terminating on the north-west at the edge of the great sea-clitl
(975 feet), and ending off on the south-east in that strange well-
known mountain-wall (1272 feet high) which rises in a sheer cliff
nearly 300 feet above the basalt-plateau on the one side and more
than 400 feet on the other. The total length of the Scur ridge is
two miles and a quarter, its greatest breadth 1520, its least breadth
350 feet. Its surface is very irregular, rising into minor hills and
sinking into rock-basins, of which nine are small tarns, besides still
smaller pools, while six others, also filled with water, lie partly on
the ridge and partly on the basaltic plateau. No one, indeed, who
looks on the Scur from below, and notes how evenly it rests upon
the basalt-plateau, would be prepared for so rugged a landscape
as that which meets his eye everywhere along the top of the ridge.
Two minor arms project from the east side of the ridge; one of
these forms the rounded isle called Beinn Tighe (968 feet), the other
the hill of A chor Bheinn.
Singular as the Scur of Eigg is, regarded merely as one of the
landmarks of the Hebrides, its geological history is not less peculiar.
The natural impression which arises in the mind when this moun-
tain comes into view for the first time is, that the huge wall is part
of a great dyke or intrusive mass which has been thrust through
the older rocks*, It was not until after some tmne that the influence
of this first impression passed off my own mind, and the true struc-
ture of the mass became apparent.
The ridge of the Scur, though formed of one great mass of rock
* Hay Cunningham, in the paper before quoted, remarks :—‘“ In regard to
the relations of the pitchstone-porphyry of the Sctr and the trap-rocks with
which it is connected, it can, after a most careful examination around the whole
~ mass, be confidently asserted that it exists asa great vein which has been erupted
through the other Plutonic rocks—thus agreeing in age with all the other pitch-
stones of the island.” Macculloch leaves us to infer that he regarded the rock
of the Scur to be regularly interstratified with the highest beds of the dolerite
series (‘ Western Isles,’ i. p. 522). Hugh Miller speaks of the Scir of Rigg as
“resting on the remains of a prostrate forest.”—Crwise of the Betsy. p. 32.
yee
304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
very different from those around it, in reality consists of two dis-
tinct varieties of rock, pitchstone and felstone-porphyry, arranged
in distinct and, in a general sense, horizontal beds. Looked at from
the east side (Pl. XIV. fig. 1) this feature is not clearly marked ;
for the great cliff seems then to consist of one homogeneous mass,
except a marked columnar band running obliquely along the base of
the precipice. If, however, the side is viewed from the south, the
bedded character of its component rocks becomes a conspicuous fea-
ture. Along the noble cliffs on that side the two varieties of rock
are strongly distinguished by their contrasting colour and mode of
weathering, the sombre-hued pitchstone standing up in a huge pre-
cipice striped with columns, and barred horizontally with bands of
the pale-grey porphyry, which seems sunk into the face of the cliff.
At the south-east end of the ridge the beds are very distinct.
Further west of the precipices to the south of the Loch a Bhealaich, the
dark pitchstone which forms the main mass is divided by two long pa-
rallel intercalations of grey porphyry, and two other short lenticular
seams of the same material (see Pl. XIV. figs. 2& 3). It is clear from
these features, which are not seen by most travellers, who pass Higg
merely in a steamer, that the Scur is in nosense of the word a dyke.
But although the Scur is thus a bedded mass, the bedding is far
different from the regularity and parallelism of that which obtains
among the interbedded basalt-rocks below. Even where no interve-
ning porphyry occurs, the pitchstone can be recognized as made up of
many beds, each marked by the different angle at which its columns
lie. And when the porphyry does occur and forms so striking a
division in the pitchstone, its beds die out rapidly, appearing now
on one horizon, now on another, along the face of the cliffs, and
thickening and thinning abruptly in short distances along the line of
the same bed. Perhaps the best place for examining these features
is at the Bhealaich, the only gully practicable for ascent or descent,
at the south-eastern face of the ridge.
By much the larger part of the mass of the Scur consists of pitch-
stone. Asa rule this rock is columnar, the columns being much
slimmer and shorter than those of the basalt-rocks. They rise
sometimes vertically, and often obliquely, or project even horizon-
tally from the face of the cliff. They are seldom quite straight,
but have a wavy outline; and when grouped in knolls here and there
along the top of the tidge, they remind one of gigantic bunches of
some of the palozoic corals, such as Lethostrotion. In other cases
they slope out from a common centre, and show an arrangement not
very unlike that of a Highland peat-stack.
The pitchstone of the Scur differs considerably in petrographical
character from any other of the pitchstones of the island, and indeed
from any other pitchstone which I have yet met with in Scotland.
Its base is of a velvet-black colour, and is so much less vitreous in
aspect than ordinary pitchstone as to have been described by Jameson
and later writers as intermediate between pitchstone and basalt*.
* “Mineralogy of the Scottish Isles,’ vol. i. p. 47. See also Macculloch, ‘ West-
ern Isles,’ vol. i. p. 521, and Hay Cunningham, ‘Mem. Wern. Soe.’ vol. viii, p. 155.
1871.] GEIKIE—TERTIARY VOLCANIC ROCKS. 305
It has a minutely granular texture, and is usually strongly por-
phyritic, with crystals of orthoclase, sometimes a quarter of an inch
in length.
That portion of the mass which forms the eastern end, or Scur
proper, shows under microscopical examination a much less perfect
glass than any of the veins above described. With a + object-
glass the rock seems to be made up of a confused aggregate of
short pale fibres or hairs matted together. These are much more
minute, and proportionally thicker than the hair-like bodies in the
veins, and they are so abundant as to form apparently the whole or
nearly the whole of the rock. At the opposite extremity of the ridge,
the rock of Beinn Bhreac is less porphyritic. Examined with the
microscope it shows a similar, but rather coarser texture, through
which, in addition to the orthoclase, there are diffused small crystals
of a delicately striated felspar*.
The grey porphyry, which occurs in beds and forms a subordinate
part of the mass of the Seir ridge, is usually a somewhat decomposed
rock. Where a fresh fracture is obtained it shows a fine-grained,
sometimes almost flinty, grey felspar base containing clear gra-
nules of quartz, and facets of a glassy felspar, probably orthoclase.
In some places the rock is strongly porphyritic. Although the line
Fig. 9.—Section at the base of the Scr of Higg (east end).
\e
)
of separation between this porphyry and the pitchstone is usually
well defined, it is sometimes so obscure, and the two rocks so shade
* The notes given above of the microscopic structure of the Eigg pitchstones
are the results of merely a preliminary examination. I hope to be able even-
tually to form materials for an essay on the minute structure of the pitchstones
of Scotland.
306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5,
into each other, that it is then difficult to regard the porphyry as
other than a peculiar and decomposed modification of the pitchstone.
This is particularly to be observed under the precipice at the east
end of the Sctr. At that locality the pitchstone is underlain by a
band of very hard flinty porphyry, varying in colour from white
through various shades of flesh-colour and brown into black, con-
taining a little free quartz and crystals of glassy felspar. Where it
becomes black it passes into a rock like that of the main mass of the
Scur. Such pitchstone parts of the bed look like kernels of less-
decomposed rock. The lower six feet of the porphyry are white and
still more decomposed. The relation of the mass is shown in fig. 9,
where the basalt-rocks of the plateau (a) are shown to be cut
through by basalt dykes (6, 6), and overlain by the porphyry (c) and
the pitchstone (d). In the porphyry are shown several pitchstone
kernels (p, p). It is deserving of remark also that in different
parts of the Scur, particularly along the north side, the bottom of
the pitchstone beds passes into a dull grey earthy porphyry, like
that now under description. Reference has already been made to
the occurrence of the pitchstone vein at Laig road along with quartz-
iferous porphyry, and also of similar porphyry and pitchstone filling
the same vein at Rudh an Tangairt. Hence, between these two
rocks there appears to be in Higg a close relationship both as to
origin and age.
Although the Sctr of Eigg is thus evidently the product of dif-
ferent flows, subsequent to the eruption of the highest of the now
visible basalt-beds, it was separated from these latter eruptions by
an enormous lapse of time. ‘This point, which is as yet a unique
feature in Hebridean Geology, I was so fortunate as to ascertain
during my survey; and though I have elsewhere* announced the
fact, I wish now to adduce the evidence upon which the conclusion
is based. My observations show that what is now the great ridge
of the Scur was formerly a river-valley, that this valley was filled
with successive flows of pitchstone-lava, that this river-silt, gravel,
and drift-wood were buried under the eruptions, and that after long
subsequent denudation the surrounding hills have been worn away,
and the river-valley, by virtue of the superior permanence of the
vitreous lava which occupied its course, has been left standing now
as the highest ridge of the district.
A little attention to the form of the bottom over which the rocks
of the Scur have been erupted suffices to reveal the fact that be-
tween the basalt-beds of the plateau and the pitchstone sheets of
the Scur there is a marked discordance, since the latter lie upon a
denuded surface of the former. Let us take a section at any part
of the ridge, and this feature will be made clear. At the little
tarn of the Bhealaich, already referred to, a section may be seen,
where the base of the pitchstone on the north side is at least
200 feet above its base on the southside. Here, as everywhere else,
the basalt-veins are abruptly cut off along the denuded surface on
* See my ‘Scenery of Scotland viewed in connexion with its Physical Geo-
logy,’ p. 278.
1871. ] GEIKIE—TERTIARY VOLCANIC ROCKS. 307
which the pitchstone rests. Again, at the east end of the Scur the
pitchstone wall is placed not fairly on the crest of the dolerite-
plateau, but on the south side of it. This cannot fail to arrest the
notice of every observer, even from a distance (see Pl. XIV. fig. 1).
It shows us not only that the rocks of the Scur were erupted along
a hollow or valley, but that only the north or north-eastern side of
that valley is now preserved.
Allusion has been already made to two minor tongues of pitch-
stone which project to the north-east from the main ridge of the
Sctr, and form small hills. Even in these offshoots the same
evidence of want of sequence between the rock of which they are
composed and the underlying basaltic sheets is clearly exposed. In
Beinn Tighe, for instance, the northern projection, a section taken
across the isle from east to west shows the basalts at a much
higher level on the one side than on the other. These offshoots
appear to have been originally either recesses of the main valley, or
tributary valleys descending into it, and to have been buried and
preserved under portions of the coulées of the pitchstone lava which
overflowed from the main mass.
Underneath the eastern end of the precipice of the Scur, on its
southern or lower side, a bed of fragmentary materials is found to
intervene between the pitchstone and the dolerites. The base of
the pitchstone dips into the hill, forming the roof of a small cave.
The under surface of the pitchstone is tolerably smooth, but undu-
lating, and shows the ends of the columns as a polygonal reticu-
lation over the roof. The breccia is a pale-yellow or grey felspathic
rock, like the more decomposing parts of the grey porphyry of the
same cliff. Through its mass are dispersed great numbers of angular
and subangular pieces of pitchstone, some of which have a striped
texture. Fragments of basalt, red sandstone, and other rocks are
rare; and the bed suggests the idea that it is a kind of brecciated
base or flow of the main pitchstone mass. A similar rock is found
along the bottom of the pitchstone on both sides of the ridge (c¢, in
fig. 9). At some points where this breccia is only a yard or two
in thickness, and consists of subangular fragments of the various
dolerites and basalts of the neighbourhood, along with pieces of red
sandstone, quartz-rock, clay-slate, &c. The matrix is in some
places a mass of hard basalt débris; in others it becomes more cal-
careous, passing into a sandstone or grit in which chips and angular
or irregular-shaped pieces of coniferous wood are abundant*. A
little further east, beyond the base of the Scur, a patch of simi-
lar breccia is seen, but with the stones much more rounded and
smoothed, This outlier rests against the denuded ends of the ba-
* The microscopic structure of this wood was briefly described by Witham
(Foss. Vegetables, p. 37), and two magnified representations were given to show
its ‘coniferous character. Lindley and Hutton further described it in their
‘ Fossil Flora,’ naming it Pinites eiggensis, and regarding it as belonging to the
Oolitic series of the Hebrides—an inference founded perhaps on the erroneous
statement of Witham to that effect. William Nicol corrected that statement by
showing that the wood-fragments occurred, not among the “lias rocks,” but
‘among the débris of the pitchstone” (Hdin. New Phil. Journal, xviii. p. 154):
i one ogi
Set al le
308 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
salt-beds forming the side of the hill. Its interest arises from the
evidence it affords of the prolongation of the old valley eastward,
and consequently of the former extension of the precipice of the
Sctr considerably beyond its present front.
It is at the extreme north-western extremity of the pitchstone
ridge, however, that the most remarkable exposure of the ancient
river-bottom is now to be seen. Sweeping along the crest of the
plateau the ridge reaches the edge of the great precipice of Bideann
Boidheach, by which its end is truncated, so as to lay open a sec-
tion of the gravelly river-bed along which the pitchstone flowed.
The accompanying diagram (fig. 10) represents the natural sec-
tion there exposed. Rising over each other in successive beds, with
Fig. 10.—Natural Section at the Cliff of Bideann Boidheach, north-
west end of the Scur of Hugg.
con
wht oil
es
Nn \
Gi) Ay
TTL Tip a
| Yi) i Vy
F Aiea i) Yy | fi
oa
=f ] tie 7
| + i 4D «
Hy ) NOT NA
Seen aN
ENON AN Nth TNA
a “ee 0% om ai eR “TNT G
Vl)
mena a
——= >
|e
ay —|
NABI SS aes? SES
«a. Bedded dolerites and basalts. 66. Basalt dykes and veins. c. Ancient:
river-bed filled with conglomerate. p. Pitchstone of the Setr.
Hay Cunningham, in the paper already cited, states that the fossil wood really hes
in the pitchstone itself! The actual position of the wood, however, in the breccia
and conglomerates underlying the pitchstone is beyond all dispute. Ihave my-
self dug it out of the bed. The geological horizon assigned to this conifer, on
account of its supposed occurrence among Oolitic rocks, being founded on error,
no greater weight can be attached to the identification of the plant with an
Oolitic species. Our knowledge of the specific varieties of the microscopic struc-
ture of ancient vegetation is hardly precise enough to warrant us in definitely
fixing the horizon of a plant merely from the examination of the minute texture
of a fragment of wood. From the internal organization of the Eigg pine, there
is no evidence that the fossil is of Oolitic age. From the position of the wood
above the dolerites and underneath the pitchstone of the Sctr it is absolutely
certain that the plant is not of Oolitic but of Tertiary date.
1871.) GEIKIE—TERTIARY VOLCANIC ROCKS. 309
a hardly perceptible southerly dip of 2°, the sheets of dolerite, ana-
mesite and basalt form a mural cliff about 700 feet high. Nowhere
in the island can the bedded character of these rocks and their alter-
nation of compact, columnar, amorphous, and amygdaloidal beds be
more strikingly seen. They are traversed by veins and dykes of an
exceedingly close-grained, sometimes almost flinty, basalt. But the
conspicuous feature of the cliffis the hollow which has been worn
out of these rocks, and which, after being partially filled with coarse
conglomerate, has been buried under the huge pitchstone mass of the
Setr. The conglomerate consists of water-worn fragments, chiefly
of dolerite and basalt, but with some also of the white Oolitic sand-
stones, imbedded in a compacted sand derived from the waste of the
older volcanic rocks. The grey porphyry, so conspicuous at the
east end of the Scur, here disappears and leaves the conglomerate
covered by one huge overlying mass of pitchstone.
An examination of the fragments of rock found in the conglomerate
on which the great pitchstone ridge of Eigg stands, affords us some
indication of the direction in which the river flowed. The occurrence
of pieces of red sandstone, which no one who knows West-Highland
geology can fail to recognize as of Cambrian derivation, at once
makes it clear that the higher grounds from which they were borne
could not have lain to the south or east, but to the north-west or
north. From the fragments of white sandstone we may with some
probability infer that the course of the stream came from the north,
where the great white Oolitic sandstones rise tothe surface. In
short, there seems ‘every probability that this old Tertiary river
flowed southward through a forest-clad region, of which the red
Cambrian mountains of Ross-shire and the white sandstone cliffs of
Raasay and Skye are but fragments, that it passed over a wide and
long tract of the volcanic plateau which has been so worn away that
it now remains in mere islets left standing out of the deep Atlantic,
that since then mountain and valley have alike disappeared, and that
in Kigg a fragment of the river-valley has been preserved solely be-
cause it has been sealed up under streams of vitreous lava which
could better withstand the progress of waste. Thus the Scur of Eigg,
like the fragments of the older basalt-plateaux of Auvergne, remains
as a monument, not only of volcanic eruptions, but of a former land-
surface, now effaced, and of the irresistible march of those slow and
seemingly feeble agencies by which the denudation of a country is
effected.
4, Summary of the Volcanic Geology of Figg.
In conclusion let me briefly summarize the more important con-
tributions made by the geology of Eigg to the history of the Ter-
tiary volcanic rocks of Britain.
1. The volcanic rocks of this island rest unconformably upon
strata of Oolitic age.
2. They consist almost wholly of a succession of nearly horizontal
interbedded sheets of dolerite, anamesite, and basalt, forming an
‘ihtnall
alia
310 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5,
isolated fragment of the great volcanic plateau which stretches in
broken masses from Antrim through the Inner Hebrides.
3. These interbedded sheets are traversed by veins and dykes of
similar materials, the dykes having the characteristic north-westerly
trend with which they pass across the southern half of Scotland and
the north of England. Veins of pitchstone and felstone, and intru-
sive masses of quartziferous porphyry, like some of those which in
Skye traverse or overlie the lias, likewise intersect the bedded basalt-
rocks of Hige.
4, At least two widely separated epochs of volcanic activity are
represented by the volcanic rocks of Eigg. The older is marked by
the bedded basalts and by the basalt veins and dykes, which, though,
strictly speaking, younger than the bedded sheets which they inter-
sect, yet probably belong to the same continuous period of volcanic
action. The later manifestations of this action are shown by the
pitchstone of the Sctr. Before that rock was erupted, the older ba-
saltic lavas had long ceased to flow in this district. Their succes-
sive beds, widely and deeply eroded by atmospheric waste, were here
hollowed into a valley traversed by a river, which carried southward
the drainage of the wooded northern hills. Into this valley, slowly
scooped out of the older volcanic series, the pitchstone and porphyry
coulées of the Scur flowed. Vast, therefore, as the period must be
which is chronicled in the huge piles of volcanic beds forming our
basalt-plateaux, we must add to it the time needed for the excava-
tion of parts of those plateaux into river-valleys, and the concluding
period of voleanic activity during which the rocks of the Scur of
Eigg were poured out.
5. Lastly, from the geology of this interesting island we learn,
what can be nowhere in Britain more eloquently impressed upon
us, that, geologically recent as that portion of the Tertiary period
may be during which the volcanic rocks of Eigg were produced, it is
yet separated from our own day by an interval sufficient for the
removal of mountains, the obliteration of valleys, and the excavation
of new valleys and glens where the hills then stood. The amount
of denudation which has taken place in the Western Highlands since
Miocene times will be hardly credible to those who have not ade-
quately realized the potency and activity of the powers of geological
waste. Subterranean movements may be called in to account for
narrow gorges, or deep glens, or profound sea-lochs; but no sub-
terranean movement will ever explain the history of the Scur of
Kigg, which will remain as striking a memorial of denudation as it
is a landmark amid the scenery of our wild western shores.
DESCRIPTION OF PLATE XIV.
Fig. 1. View of the Sct of Hige from the east.
2. View of the Scir from the south.
3. View of the precipice of the Sctr to the south-west of the Loch a
Bhealaich.
Quart. Jovan. Geol. Soc VolXXVIL PIXTV
GR DeWilde. del.et lith. 3 . Wantern Bro® fap
VIEWS OF THE SCUR OF ICG.
1871.) GEIKIE—TERTIARY VOLCANIC ROCKS. 311
Discussion.
Prof. HaveHton inquired whether Mr. Geikie’s attention had been
called to the Mourne Mountains in Ireland, which seemed to present
some analogous phenomena to those described in the paper. In the
Mourne district were dykes of dolerite, pitchstone, glossy basalt, and
other volcanic rocks of the same constitution as those of Antrim.
He believed that a chemical examination of these rocks in different
districts would prove their common origin. The evidence in Antrim
was conclusive as to their Tertiary age in Ireland; and he was glad
to find that the view of their belonging to a different age in Hige
was erroneous.
Prof. Ramsay had hitherto believed in the Oolitic age of these
trap-rocks in Higg, but accepted the author’s views. The interbed-
ding of volcanic protrusions among the Lower Silurian beds in Wales
was somewhat analogous. He was glad to find the history of these
igneous rocks treated of in so geological a manner, instead of their
being regarded from too purely a lithological and mineralogical point
of view. The great antiquity of these Middle Tertiary beds had, he
thought, been most admirably brought forward in the paper, as well
as the enormous amount of denudation; and he would recommend
it to the notice of those who had not a due appreciation of geolo-
gical time.
Mr. Forses hoped that the geologist would remember that his
father was a mineralogist. It was refreshing to find a paper of
this kind brought before the Society, as it was to be regretted
that the details of mineralogy were so little studied in this country
when compared with the Continent; and this he attributed to the
backward state of petrology (admitted by Mr. Geikie) in this
country. He quite agreed in the view of the Tertiary age of these
rocks. With regard to the terminology employed by the author, he
objected to the use of the word dolerite, as distinct from basalt ;
basalt properly comprised, not only dolerite (the coarse-grained
variety) and anamesite (the finely-grained variety), as well as true
basalt, but also tachylite (the glassy variety), which was frequently
confounded with pitchstone. All four names merely referred to
structure, and not to composition.
Mr. Gerxtm, in reply, stated that he had not examined the Mourne
Mountains. He had not in any way wished to disparage mineralogy,
but, on the contrary, had attempted to classify the different rocks
according to their petrographical characters. He used the term do-
lerite in the same sense as the German mineralogists, both as the
generic name for the whole series, and also for the coarser variety
of basalt.
pe
312 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5,
4, On the Formation of “ Crravzs,” and their bearing upon THEORIES
attributing the Excavation of ALPINE VaLLEYs mainly to the
Action of Guacters. By the Rev. T. G. Bonny, M.A., F.G.S,
Tue following paper is an attempt to examine how far a theory
which during the last few years has obtained more or less support
from many very eminent geologists, can be applied to one of the most
remarkable features in several mountain-valleys. Although “ cirques”
are more commonly associated with the Pyrenees, they are by no
means infrequent or on a small scale in the Alps; and as I know
the former mountain-chain only at second hand, I shall confine my-
self to the latter, and to those instances which I have personally ex-
amined.
In venturing to treat of a subject so full of difficulty, and to op-
pose the opinions of persons far more eminent than myself, I may
venture to plead as my excuse that I do not write without some ex-
perience of mountain-regions, seeing that I have twelve times visited
the Alps, have wandered, generally on foot, over almost the whole
chain, and have had during many of these journeys this subject of °
mountain-sculpture especially present before my mind, so as to be
constantly on the watch for evidence bearing upon the various
theories that have been advanced.
First let me briefly describe a few of the most remarkable cirques,
beginning with the Creux de Champs.
This is an approximately semicircular amphitheatre on the northern
face of the Diablerets, forming the head of a short glen terminating the
valley of La Grande Eau, which joins the Rhone at Aigle. Vast preci-
pices of limestone and shale enclose it, which are crowned with short
wide glaciers, and surmounted by the blunt peaks of the Diablerets,
the highest of which reaches an elevation of 10,666 feet above the
sea. The floor of this glen, though encumbered with moraine stuff,
and intruded upon by the great, taluses beneath the precipices, is
tolerably level, and is probably about 4000 feet above the sea*.
Above the slopes an almost unbroken wall of limestone rock rises
for at least 2000 feet ; shales, alternating with narrower bands of
limestone, then reduce the precipitousness and produce the ledges
whereon the glaciers rest ; and, finally, the limestone peaks rise like
broken battlements on the summit of the wall. From these snow-
laden ledges numerous streams gush down the rock, some mere white
threads of spray, others turbid cascades, whose volume varies with
the hour of the day and the state of the weather. Speaking in
general terms, we may say that for an are of about 80° this cirque
is enclosed by a nearly vertical wall of precipices rising full 5000 feet
above its comparatively level floor. The strata exposed, though here
and there contorted, and in one place at least folded, lie on the whole
pretty evenly, and appear to dip gently a little south of west.
The Fer-a-Cheval.—This cirque differs from that last described in
being situated just on one side of a large peak, and in opening into
* The Hotel des Diablerets, at its mouth, is 3832 feet ; and the fall of the val-
ley-bed is not rapid.
1871.] BONNEY—FORMATION OF “ CIRQUES.” 313
rather than forming the head of a valley; it is really a semicircular
recess in one of its walls, between the towers of the Pointe de Tenne-
verges and the lower summit of the Téte Noire.
The base of the former mountain consists of a vast mass of com-
pact limestone, which also (as in the former case) sweeps round the
cirque in a wall of precipices full 1000 feet, and often more, in
height. This, in the Pointe de Tenneverges, is surmounted by slopes,
marking doubtless the presence of more shaly strata; and these are
capped by another vast mass of limestone with more frequent
partings, which is crowned by the actual peak. Above the wall of
the cirque, and excavated in the lower part of this limestone and in
the subjacent shale, is an upland glen which leads up to the Col de
Tenneverges (8154 feet).
In the neighbourhood of the Fer-i-Cheval, as in the Creux de
Champs, the strata, though occasionally locally contorted, are on the
whole tolerably horizontal; and it too is remarkable for the number
and beauty of its waterfalls. In the spring and early summer,
‘every notch along the serrated line of crag becomes the birth-
place of a waterfall, from the tiny thread of spray which quivers in
every breeze and dances irresolutely down the sombre crag, to the
furious torrent plunging in one bold leap from top to bottom of the
deepest precipice, and announcing its presence with a voice that
emulates the thunders of the sky” (Writs, The Eagle's Nest,
p. 34)*.
The Croda Malcora.—The cirque of the Croda Malcora, high up
among the crags of the dolomitic mass that culminates in the
Sorapis, has been termed “ another Gavarnie” by Messrs. Gilbert
and Churchill}, though to myself it appeared to present the di-
stinctive features. of a cirque less conspicuously than the two de-
scribed above. +Its rocky floor is broken into a series of irregular
steps, supporting some patches of snow and glacier ; it is, however,
enclosed by a magnificent wall of dolomitic crags, probably not less
than 1000 feet in height. The cascades here, so far as I remember,
can only be conspicuous after heavy rain or in the spring time ; for
in summer the upper crags are almost bare of snow, and dry. Time
did not allow me to enter it; but I obtained an excellent view into
it from a short distance away. The same district of the Ampezzo
offers several instances of glens with a cirque-like formation ; among
these are one of no great size but with steep sides, nestling beneath
the great peaks of Monte Tofana, and a most singular one, well seen
from the summit of that mountain, termed the Croda di Lagazoi,
which I can only compare to a rude amphitheatre with walls of rock
instead of masonry, through which a complete breach has been made
at one of the vertices of the ellipse.
The Creux du Vent (Jura).—The Creux du Vent, near Noiraigue
station on the Val Travers railway, is reported to be the finest exam-
ple of a cirque in the Jura. It is thus described by Mr. Ball :—“a
* The neighbourhood, in which are several maguificent ranges of precipices,
is well described by the same author. Alpine Journal, vol. ii. p. 49.
7 The Dolomite Mountains, p. 407.
314 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
mountain nearly level at the top, which derives its name from a
singular hollow, nearly two miles in circumference and 1000 feet
deep, lying near to the summit.” To this I add my own note*.
‘It is excavated in a mass of banded limestone and shale, the strata
lying horizontally in the face of the cliff, except at the more southern
extremity, where they curve upwards. All down the cliff are dis-
tinct traces of the erosive action of many streamlets. The floor of
the valley below is a level basin, as though it had once held a lake.”
This was written at the railway station, whence there is a fine view
of the cirque.
Am Ende der Welt, Engelberg.—This cirque is at the termination
of the Horbis Thal, a glen descending into the Aa valley just above
Engelberg. Less grand than either the Fer-a-Cheval or the Creux
de Champs, it is still a striking object, and exhibits the same pecu-
liarities of a comparatively level floor, of enclosing precipices, and of
numerous waterfalls. The strata in the precipices, which are perhaps
about 1500 feet high, are moderately horizontal on either side, but
much contorted in the middle. The walls of the cirque, when it is
viewed from the lower end, appear to be crowned with sloping alps,
and these to be surmounted with a line of limestone crags. Speaking
more correctly, it forms a sudden step or break in the level of an
upland valley which lies between two great spurs of the Rothstock
massif, and carries the drainage of the Graussen glacier to the Aa.
It would be easy to multiply examples of cirque-lke glens, similar
though inferior to these ; but as they would exhibit no fresh features
of importance I pass on to my last case, which satisfied me that only
one explanation could be offered of their formation.
The Cirques of the Rothstock.—As the traveller bound from En-
gelberg for the Surenen Pass gains the rugged pastures of the
Blacken Alp (5833 feet), he sees gradually opening but on his left
hand, not one, but two fine cirques cut out of the highest part of the
Rothstock massif. They are separated by a spur from the peak
named Rothschutz on the Federal Map, and are very similar in ap-
pearance, though the eastern one is on the whole the finer of the
two. Its other extremity is the Blackenstock (9587 feet), and from
this summit to the Rothschutz (9278 feet) runs a line of crags not
much inferior in height. The chord joining these two points is
about 2800 yards long, and the sagitta of the are about 650 yards ;
but the spurs projecting from the two extremities give a more semi-
circular appearance to the cirque than these measurements would
suggest.
Above the usual taluses of débris rises a high band of cliffs of a
hard yellowish-grey limestone, which supports a still loftier belt of a
reddish rock, doubtless a rather sandy and coarse calcareous shale ;
over this is a sort of terrace-shelf or slope, hollowed out into small
combes ; and then rises another barrier of limestone cliffs, forming the
ip of the cup-like hollow. Clouds prevented me from seeing the
sky-line in more than one place; but it is nowhere more than a few
hundred feet below the peaks named above. For the same reason, I
* Central Alps, p. 5.
1871.| BONNEY—FORMATION OF “ CIRQUES.” 315
cannot attempt to give any accurate estimate of the height of the
cliffs; but the two lower stages appeared to me together not less
than 500 feet. The strata lay tolerably horizontal, only curving
upwards somewhat in the western part of the western cirque. The
Fig. l.—Rough sketch of Cirque mm Rothstock.
Pig ft eee’ =
a ee ee
eh * fae a
A. Clouds concealing peaks. B. Limestone cliffs. C. Shaly slope, with
small combes and snow-beds. D. Shaly cliffs furrowed by streamlets.
HE. Limestone cliffs, occasionally slightly grooved by streamlets. F.
Floor of cirque with talus-heaps at side,
most remarkable thing about the cliffs was the belt of reddish shaly
rock, which was furrowed by a vast number of little gorges, which
were often only a few yards apart and occasionally united, so that
this part of the cliff really looked like a badly ploughed field set up
on end. Down these gorges, many of them dry in August, little
rills descend from the snows on the ledges and in the combes above,
which have generally made some trace corresponding with their size
on the harder limestone below—sometimes a mere stain, sometimes
a well-marked groove.
What explanation, then, are we to give of these rocky recesses with
their steep, almost vertical sides, and floors often comparatively level ?
To avoid misconception, let me premise that in adopting any one
explanation, I do not mean to absolutely exclude all others, but
merely select the one which above all others accounts for the exist-
ing physical features. Thus, for example, were I to attribute a valley
to the erosive action of a glacier, I should not intend to exclude up-
heaving forces,-denudation by waves, currents, and rivers, d&c., all
of which may have had much influence in preparing the surface for
the glacier, but only mean that the glacier has effaced all, or almost
all, the tool-marks of these preceding agencies—just as, when speak-
ing of a statue as carved by a chisel, we take no note of the crow-
bars, wedges, picks, blast-powder, and other appliances which were
employed to quarry the block before it was placed in the sculptor’s
hands.
316 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
(1.) I dismiss at once any theory of “craters of upheaval,” by
which some distinguished geologists have attempted to account for
valleys which approach the cirque form, such as that of La Berarde*,
because, after examination of this and many others, I can conceive of
no theory of upheaval or fracture which could leave them in a state
at all resembling their present one. That a valley like the one at
La Berarde, to say nothing of these cirques, should be a “ crater of
elevation’ appears to me a physical impossibility.
(2.) Can these cirques be explained by any theory of marine
erosion, and compared with the coves which we not unfrequently find
on the sea-coast? Though possibly this explanation might be applied
to some cases, I do not think it will fit all or nearly all that exist.
After seeing how little effect the sea has in the Fjords of Norway,
I cannot attribute the Fer-a-Cheval or the Creux de Champs in these
remote and sheltered valleys to marine erosion, whatever effect the
waves may once have had in blocking out the main features of the
Alpine peaks.
(3.) Can we call in the intervention of glaciers, now so muck in
favour as nature’s carving-tools among geologists ? and may these
cirques be regarded as results of what Mr. Ruskin would call “ minor
fury of ice-foam” +? Weshall perhaps best answer the question by
considering first this particular case :—whether, assuming that glaciers
have been principal agents in the excavation of Alpine valleys, we
can suppose the cirques to have been formed by them ; and second,
whether the assumption just made, that glaciers have been principal
agents in the excavation of Alpine valleys, is a correct one. Now,
if these cirques are the result of glacial erosion, they were either
fashioned (a) by a glacier which took its rise in them, or (6), like the
concavities in the course of a river, by the action of a passing ice-
stream. The first of these suppositions appears to me physically
impossible. Granting, as we must do, to begin with, some kind of
hollow or slight combe on the mountain-side in which the snows
could collect and form a névé, the erosive action on this part would
always be very slight (for the ice here is less compact than that below) ;
the friction would be that due to the weight alone of the superin-
cumbent ice ||, and, what is most important, there is but little grit
between it and the subjacent rock ; for comparatively few stones are
_ engulfed in the névé of a glacier. I can conceive it possible that if
a glacier, after wearing away a stratum of hard rock, reached one
in which erosion proceeded more rapidly, it might deepen its angle
of descent to some degree in the upper stratum also; but I cannot
conceive that precipices more than a thousand feet high could be thus
* In Dauphiné. See Forbes’s ‘ Norway and its Glaciers,’ p. 259.
+ My own examination of mountains has led me to conclusions very different
from those advocated by Mr. Mackintosh in his ‘Scenery and Geology of England
and Wales,’ although I think it possible that some peaks and ranges may have
originated in insular fragments.
{ Geol. Mag. vol. ii. p. 50.
|| Friction Gc normal pressure; in many of the lower parts of a glacier,
normal pressure at any point = weight of column of ice above that point + a
pressure derived from ice behind.
1871.] BONNEY—FORMATION OF ‘ CIRQUES.” 317
produced ; and we must remember that in the most conspicuous of
those described above, the most compact rock forms the lowest stage.
To this question of cliffs in the bed of a glacier I shall return again;
for the present we may venture to assert that it is mechanically im-
possible for a glacier to sink into its bed so as to excavate a cirque
on so gigantic a scale. (6) But may they have been produced at some
bend in the ice-stream like the concavities in a river’s course? The
Creux de Champs and Am Ende der Welt certainly cannot be thus
explained, because they are at the head of deep well-marked lateral
glens about a mile and a half long. The two cirques near the
Blacken Alp are inexplicable on this theory ; for the spurs from the
Blackenstock and Rothschutz would effectually shelter them from the
action of any glacier descending from the Surenen Pass (7562 feet);
and indeed the general contour of the ground suggests that their re-
cesses would be among the feeders of its névé, the rise from the
Blacken Alp to the last ridge leading to the Pass being comparatively
gentle. The Fer-i-~Cheval would offer less resistance to this expla-
nation than any other cirque, as it is on the concave side of the elbow
of a valley; but as existing glaciers do not appear to produce such
marked effects in turning corners in their present beds, we may
fairly require much corroborative evidence before venturing to apply
this explanation here.
There remains then the wider question to consider, Are we jus-
tified in supposing glaciers to have been the principal agents in the
excavation of the Alpine valleys? To prevent mistakes, let me state
that I do not now purpose to deal with that particular case of this
theory which is advocated by several distinguished foreign geologists,
and with so much ability in this country by Professor Ramsay, viz.
the excavation of lake-basins by glaciers, but rather with that wider
view to which, among others, Professor Tyndall has more than once
given the support of his experience and talent, especially in a paper
published in the Philosophical Magazine*.
If we assign to glaciers any large share in the excavation of val-
leys, we may fairly ask that the main contours should lend them-
selves readily to this explanation, just as those of a river-valley,
although somewhat modified by other meteoric action, suggest run-
ning water as the tool that has principally fashioned them. Now,
as a rule, in the upper parts of Alpine valleys, where the glacial
action may be supposed most recent, and therefore least affected by
other denuding agents, we are struck by the steepness of the last
few miles up to the watershed, as compared with the inclination of
the rest of the bed. I will only mention a few instances out of
many—for the fact must have struck all travellers—and will select
the first from the Dauphiné Alps, not only because it is a district
very familiar to myself, but also because the valley of the Vénéon
runs, for its whole extent, with one most unimportant exception,
through remarkably hard crystalline rocks. Measured on the map,
this valley is about twenty miles in length from the spot where
the river debouches into the small plain above the Romanche, near
* Phil. Mag. Ser. 4. vol. xxiv. p. 169.
VOL. XXVII.—PART I, a
318 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
Bourg d’Oisans, to the head of the Glacier de la Pilatte. This
glacier occupies an extensive glen, guarded on one side by the huge
precipices of the Ailefroide (12,877 feet), on the other by a nameless
mass, the highest peak on which is probably about 12,000 feet. The
lowest point in the loop-like créte connecting these two portals is
about 10,800* feet above the sea. The exact height of the foot of the
glacier I do not know; but probably 6800 feet is an estimate rather
above than below the truth; for the ascent from La Bérarde (5702
feet), 34 miles down the valley (on map), is not great. Measuring
in the same way, it isjust two miles from the Col du Sélé to the foot
of the glacier (=10,560 feet). Neglecting the odd hundreds, which
we are justified in doing, as the lower part of the glacier is flat, we
have a fall of 4000 feet in 10,000 feet. From La Bérarde to St.
Christophe, 62 miles (=35,640 feet), the fall is 879 feet, nearly
25 in 1000 feet. From the latter place to Venose (3363 feet), a
distance of about 32 miles, the fall is 1460 feet; and from Venose to
the opening of the valley, perhaps about 43 miles, the fall must be
950 feet ; for the descent afterwards to Bourg d’Oisans (2380 feet)
is but slight. The fall of the valley between La Beérarde and St.
Christophe is rather more than is given by the difference of the two
stations, as the latter place stands some height above the stream,
and this may a little affect the next measurement below.
The result of this is, that the fall of the valley-bed during the
first two miles (measured on the map) is 40 in the 100, and
after that, for the remaining 17 miles of its course, its fall is
always considerably less than 10 in 100. Moreover, in that
uppermost portion, the slope very perceptibly increases as the
watershed is approached, so that the last few hundred feet, whether
of snow or rock, are of formidable steepness, the ascent to the
only accessible point (the Col du Sélé) being a stiff bit of rock-
climbing. The same configuration is exhibited by most of the tri-
butary glens that join the main valley—by one, the Vallon de la
Bonne Pierre, leading up to the Col des Kcrins, to an even greater
degree. Three of these are of considerable sizef, and must in
former times have brought down immense tributary glaciers ;
they join the main valley at or below La Bérarde; and yet there is
not any marked deepening or widening of the valley caused by the
great increase of the ice-stream.
Take, again, the glacier on the north side of the créte of the
Rateau (fig. 2) ; how could it have excavated that cliff which rises
full 2000 feet above it? while, as if to make the puzzle greater,
within a mile to the west, begins the Glacier du Mont de Lans, which
covers a vast plateau, about 11,000 feet in height, sloping gently
to the north. Here the glacier reclines like a white cloth upon a
table, protruding a few tongues of broken ice into two or three
comparatively shallow notches that have been worn out in its
northern edge.
* The Col du Sélé is 10,814 feet, mean of B. P. (Tuckett) and Bar. ( W.
Mathews) ; and several other parts of the ridge are of much the same height.
t The Vallons des Etancons, de la Muande, and de la Selle.
1871.] BONNEY—FORMATION OF “ CIRQUES.” 319
Fig. 2.—Diagram of Le Rdteau.
P. Precipice of Le Rateau. P’. Rocky Spurs with precipices towards Glacier,
S. Steep snow slopes. G, Glacier. =—> Snow-basin leading to Gla-
cier du Mont de Lans,
If, then, it be conceded that the névé of a glacier can settle down
so fast that the uppermost mile or two of its bed shall be almost a cliff
compared with the remainder of the stream, and we thus account
for the configuration of such valleys as those above named, and, on
a smaller scale, those in which lie the Brenva, Miage, and Argenticre
glaciers near Mont Blanc, the Unter-Grindelwald and Lauter Aar
glaciers in the Oberland, the Trift glacier near Zermatt, and dozens
more which could be easily named in all parts of the Alps, how are
we to explain such contradictions as the Mont de Lans, the Théo-
dule, the Gorner (between Monte Rosa and the Strahlhorn), and the
Tiths glaciers? or such anomalies as the low opening of the Am-
pezzo Pass (about 5000 feet) among the towering summits of the
Drei Zinnen, Cristallo, and Geiselstein*? Surely it is far safer to
suppose that the glen, by whatever cause fashioned, gave rise to the
glacier, rather than the glacier to the glen.
But perhaps it will be urged that the greater steepness of the
heads of the valleys may be explained by the fact that, in the gra-
dual retreat of the ice-streams since the glacial epoch, they have
been exposed to erosive action for a longer time than the lower
parts; and so the glaciers, in comparatively recent periods, have
steepened the slope of their upper glens. The suggestion is plausi-
ble, and might be supported by an appeal to tarns like those of the
Lago Bianco and Nero on the Bernina Pass, and by occasional flat
* All about 10,000 feet above the sea.
Loe
=
320 - PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
plains near the ends of existing glaciers, which might be presumed
to be filled-up lake-basins; still these cases of glacial erosion, if
such they be, are on a very small scale compared with the amount
of denudation that this hypothesis requires; and there are many
others, as, for example, in the Val del Campo and Val Viola*, where
the great heaps of moraine stuff show the glaciers to have long re-
mained just filling up the whole of a lateral valley, without any
marked effect on the bed behind.
This difficulty is increased when we examine the bed of an exist-
ing glacier, a thing which the rapid diminution of some of the Ober-
land glaciers during the last few years has made possible. The
surface of the Unter-Grindelwald glacier was (July 1870) about 100
feet lower, and the extremity had retreated full 500 feet higher up
the steep hill-side, than in 1858. Formerly it descended to the level
of the valley ; it now rests on a low cliff of rock; and its stream no
longer gushes out from an ice-cave, but runs deep in a rocky gorge.
This shows that the glaciation of a valley, and the cutting a gorge
in its bed may be simultaneous. (The Rosenlaui glacier affords
another example of this.) It can now be seen that the final icefall
descends over three or four steps of hard limestone; the last, and
perhaps the tallest of these, together with what we might call the
first flag of the valley-floor, being at present exposed. If, then, the
glacier has made these steps, if it is plastic enough to mould itself
to them (which it is not in all cases), surely it ought, at the base of
each wall, to have worn out considerable hollows, analogous to the
pot-holes at the foot of a cascade. But there is nothing of the
kind to be seen; the rocks, beautifully polished and scratched in
many places, exhibit the usual contours, and after forming an irre-
gular lumpy terrace, showing often ‘‘Stoss- and Leeseite,” round
away to the next cliff.
The steps, not uncommon in valleys, such as those in the Val
Formazza, and that which is visible from near Landro, in the glen
which descends from under the Drei Zinnen to the Durren See, pre-
sent similar but still greater difficulties in accepting the hypothesis
of glacier erosion.
Again, how are valleys such as those of the Pusterthal or the
Upper Etschthal, to be explained on a theory of glacial erosion? The
former is a well-marked and generally wide trench, about fifty
miles long, extending east and west from Miuhlbach, where the
Rienz turns sharp to the south, to Silliian on the Drave (to say
nothing of any further extension to the Gailthal). For the most
part it is enclosed by mountains 8000 or 9000 feet high ; and the
flat Toblach plateau, which parts these rivers and forms the water-
shed between the Adige and the Danube, is 3951 feet above the
sea, “sloping gently, almost imperceptibly,” in either direction.
No one who has seen this great trough, whose sides are steep moun-
tains, rising 4000 feet or more on either hand, whose base dips
* Valleys connecting, on the Italian side, the lower parts of the Bernina and
Stelvio Passes.
1871.] BONNEY—FORMATION OF “‘ CIRQUES.” 321
gently* from a central plateau to opposite points of the compass,
can conceive it to have been excavated by a glacier.
In consequence of these reasons, in addition to those already
advanced by Sir R. Murchison, Sir C. Lyell, Mr. Ball, M. Favre,
&c., I venture to maintain that it is impossible for glaciers to have
excavated cirques, and difficult to understand how they can have
excavated valleys. I now take one step further, and shall endea-
vour to show that, if they excavated the valleys, they must also
have excavated the cirques. Consider, for example, the case of the
Creux de Champs. This is not, as it at first sight appears, in a
lateral glen, but at the true head of the Grande-Kau valley. The
principal excavating agent, be it ice or water, must have always
followed the line of the present drainage of the cirque, and not of
that from the lower alps of the Col de Pillon.
Efface the cirque, replace in imagination the vast mass of ma-
terial which has been scooped out of the heart of the Diablerets
between Ormond Dessus and the peaks of the mountains fill up the
valley of the Grande Eau, far above the village just named to near
the level of the Col de Pillon, there will then be a rather regular
and shallow trench, bounded on the one side by the Tornette chain,
on the other by the Diablerets’ massif, a far huger block than now.
From this the western and north-western drainage, whether in a
liquid or solid form, would have descended, chiefly along the val-
leys mentioned above, and partly by the small glen west of the
Oldenhorn, which, at the present day, has a cirque-like configura-
tion, while only a little would have been supplied by the low alps
of the Col de Pillon. Any glacier, therefore, which excavated the
Grande-Eau valley below Ormond Dessus must have received its
chief ice-affluent from the direction of the present cirque ; and I am
convinced that no one who has seen the locality could ever attri-
bute the formation of the two parts of the valley above and below
this village to different agencies. If, then, we have established that
the excavation of a cirque by a glacier is mechanically impossible,
the cirque, if not prior to it, must have been excavated by some
other agent since the ice-period. But if the streams have been able
to remove this enormous amount of débris above Ormond Dessus,
how can we account for their comparative inefficiency below? If
they have been so active here, and in a few other glens, how is it
that they have been practically inactive in the Rhone valley and its
other tributaries, and in the great majority of Alpine valleys?
Above all, how are we to account for the presence of moraines in
the cirque itself?
The same remarks would apply to the Fer-a-Cheval and Am Ende
der Welt, whose floors join, were it possible, even more uniformly
with those of the main valleys, in which signs of glacial action are
still abundantly visible.
The conclusion then seems to me inevitable, that the cirques, and
* The levels of points in the valley are, Muhlbach 2542 feet, Untervintl
(9% miles) 2502 feet, Bruneck (14 miles) 2686 feet, Niederndorf (14 miles) 3784
feet, Toblach 3951 feet, Innichen 3701 feet, Sillian (14 miles) 3611 feet.
322 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 5,
therefore the valleys themselves, were mainly excavated before the
glacial epoch, and that the effect produced upon them by the glaciers
was, comparatively speaking, superficial *.
It remains therefore to ask, what agent, or agents, have pro-
duced these remarkable natural amphitheatres, and those minor
and less perfect copies so common in the limestone districts, though
not wholly confined to them ?
In the descriptions of these cirques, attention has been called to
the numerous streamlets seaming their cliffs, which were most of
all conspicuous in the two under the Rothstock peaks.
Running water, in falling over a cliff, notches the edge, grooves
the face, and undermines the base with its spray. Its action is
partly mechanical, partly chemical. If then its erosive power be
considerable (as when the stream is unusually silty), or if the rock
yield slowly to meteoric agents (such as rain and frost), it will cut
a gorge, as is commonly the case with glacier streams, and especially
in erystalline rocks.
If, however, the water be generally pure, and the rock be easily
affected by these other agents, the cliff will recede very slowly and
uniformly, as at the Staub-Bach, near Lauterbrunnen, or, at most,
will be modified into a crescentic hollow, as at the Nant Dant, near
Samoens.
If, then, we have a number of small streams acting in this way,
we shall get a cliff formed which will be either a straight wall or,
since the streams towards the middle will probably be larger and
more nearly perennial than those at the side, an amphitheatre.
The instances to which I have referred have exhibited this pro-
cess on a grand scale; the annexed diagram (fig. 3) exhibits the same
onasmall one. It is taken from a little cirque or, rather, a recess
* Two arguments often advanced to show the excavating power of glaciers
appear to me of doubtful value. The vast quantity of mud and silt borne
down by the stream from a glacier is adduced as a proof of its destructive
power ; and it is argued ‘so many cubic yards of silt deposited annually, so
many of rock removed annually from the bed of the glacier.” But is this the
fact? ‘There is often abundance of fine gravel on the surface of a glacier, which
has not come from the bed; and I am convinced that a very large portion of
the silt borne out by the stream does not come from the subjacent rock, but from
the blocks which, after being detached by frost, &c. from the mountains on either
side, fall in vast quantities upon the surface of the glacier; many of these are
engulfed on their downward passage, and must be crushed to powder in that
gigantic mill, of which the quern is rock, the rubber ice.
Again, it is assumed tacitly that as the glaciers were once enormously greater
than at present, their erosive powers would be proportionately greater. But
this may not be hastily assumed. The erosive efiect of a glacier on its bed
must surely depend far more on the grittiness of its under surface than on the
weight of the ice. A child with a bit of sandpaper would scour rust away from
iron faster than a man with a smooth rubber. Now it must be remembered
that the more the hills are covered with snow, and the valleys filled with ice,
the fewer peaks will project, and the less rock can fall upon the glacier’s
surface; and so its very bigness will make it the worse file. I believe this re-
mark to be especially applicable to a country like Scandinavia. The scouring
power of clean ice cannot be great; for Mr. Hopkins determined experimentally
that the coefficient of friction of solid ice upon rather rough sandstone was tan
20°, the same as that of polished marble.
1871.] BONNEY—FORMATION OF “ CIRQUES.” 323
high up in the limestone cliffs above the Aa-valley, on the left bank,
a short distance below Engelberg. Here six or seven small streams
issue from the rock, and have worked out a hollow only a few
dozen yards wide, yet of the true cirque type.
Fig. 3.—Smaill Cirque near Engelberg.
A. Limestone Cliffs. B. Shaly bank with some trees &c., out of which the
streams break. C. Limestone cliff. D. Cirque. s=—> Cascade.
The conditions, therefore, most favourable to the formation of a
cirque are :—
(1) Upland glens, combes or terraces, so shaped as to give rise
to and to maintain many small streams.
(2) Strata, moderately horizontal, over which these streams fall,
which, by their constitution, yield considerably to the other forms
of meteoric denudation.
(3) These strata must nevertheless allow of the formation 2
cliffs ; and thus perhaps the most favourable structure is thick beds
of limestone, with occasional alternating bands of softer rock.
Probably some favourable configuration of the ground must be
also assumed at the beginning: if a glen ended in a cliff, it would
doubtless be more readily cut into a cirque; but whether this
is always needed, or what cause has made the cliff, I do not now
attempt to investigate. I venture to submit that I have proved
that glaciers cannot have produced the cirques, and that (since
these cirques cannot be postglacial) they have not, to any great
extent, excavated the Alpine valleys. To assign to each agent its
due share in the task of erosion in the Alps (and in all other moun-
tain-regions that I have seen) appears too complicated a problem
324 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 5,
to be solved with the means at present at our disposal; my own
belief, after many years of observation, is, that subterranean forces
(whether of upheaval or depression, by folding and fracturing the
strata), sea, air, frost, rain, streams, and glaciers have all played
their part in this task of mountain-sculpture. Perhaps it may be
possible some day to approximate to the work done by the first
two; but the more I examine the Alps the more convinced I become
that the next four have been the chief agents in producing the pre-
sent configuration of their valleys, and that the effect of the last in
the list has been superficial. Harth-forces, like Titanic hands, have
moulded and broken, the sea has planed, the heat and cold have
split like wedges, rain and rivers have chiseled and sawn, while the -
glacier rasp has rounded edges and filed down protuberances, but
has done comparatively little among the harder rocks to deepen or
excavate.
[P.S. Since the above paper was read, Mr. E. Whymper’s ‘ Scram-
bles amongst the Alps’ has been published, in which are some very
important remarks upon the question of glacier-erosion. Professor
Tyndall, in his recent work ‘ Hours of Exercise in the Alps,’ appears
to speak rather less confidently with regard to his theory than in
the paper quoted above. |
Discussion.
Mr. Wuiraker suggested an analogy between the cirques and the
combes in our own limestone countries.
Mr. Gurxie regarded the cirques as analogous to the cwms of
Wales and the corries of Scotland. They were not, however, con-
fined to limestone districts, but occurred also in gneiss and granite
rocks. He thought that the shape was much influenced by the bed-
ding and jointing of the rocks, as there was an evident connexion
between these and the shape of the cwms. He could not, however,
see his way to account for the vertical cliffs surrounding the cirques.
The Rev. T. G. Bonnuy, in reply, observed that though cirques
were not confined to limestones, the finest instances occurred in such
rocks. When cirques occurred in crystalline rocks, the talus was
usually much larger than in limestone.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
POSTPONED PAPER.
On the SrructursE of the Crac-Beps of Surrotk and Norroix, with
some OBSERVATIONS on thew Orcanic Remains. By JoserH
Prestwicu, F.R.S., F.G.S., &c. Part I]1—Tue Rep Crae or
Essex AnD SUFFOLK.
(Read May 20, 1868 * .)
THe superposition of the Red Crag upon the Coralline Crag is clear.
The points on which there are some differences of opinion relate
chiefly to questions of structure and to the relation of the Crag-
beds of Suffolk with those of Norfolk. Like the Testacea of the
Coralline Crag, those of the Red Crag have been the object of
assiduous research on the part of Mr. Searles Wood}, whose list
leaves little to be added, except the more special determination of
their local distribution. To Mr. Searles Wood, jun.+, also, we are
indebted for an elaborate account of the different stages into which
he considers the deposit should be divided, to the Rev. Mr. Fisher
for a paper on its relation to the Mammaliferous Crag §, and to
Mr. 8. V. Wood for a subsequent paper on the structure of the Red
Crag||. To the paleontographical papers I shall have occasion to
refer presently.
The Red Crag of Suffolk covers an area of about 300 square miles.
It is, however, so overlain by the sands and clays of the Boulder-
clay series, that generally it is only on the sides of the valleys which
intersect the district that the Crag-beds come to the surface and
are to be seen. The places where they are best exposed are on the
slopes of the hills skirting the rivers Orwell and Deben, and in the
cliff-sections at Bawdsey and Felixstow. As before mentioned, the
Red Crag occupies an excavated area in the Coralline Crag, wrapping
round the isolated reefs of the latter, filling up the hollows between
them, and lying nearly on a level with the conterminous Coralline
Crag. Whilst the Coralline Crag consists essentially of light-coloured
calcareous beds with an admixture of siliceous sand, the Red Crag
consists of a base of siliceous sands with more or less of the peroxide
of iron and a few thin seams of clay. They form such an extremely
variable series that I have failed to observe any definite order of
succession in the various beds of the lower series, or to recognize
the “ Beach-stages ” of Mr. 8. Wood, jun. I would divide them into
two groups only—the lower one characterized by the prevalence of
* For the discussion on this paper see Quart. Journ. Geol. Soc. vol. xxiv.
p- 462.
+t Palezont. Soc. Trans. 1848-56. { Ann. & Mag. Nat. Hist. March 1864.
§ Quart. Journ. Geol. Soc. vol. xxii. p. 19. || Zbed. p. 538.
VOL. XXVII.—PART I. BP IN
326 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
oblique lamination, without permanent or definite order of succes-
sion in the beds, and the upper by more persistent horizontal bed-
ding. Shells abound in the lower, and are rarer in the upper division.
The general features of the Red Crag are too well known to
require more than brief mention. In the central area there occurs
at the base of the lower division a bed of phosphatic nodules (the
so-called “ coprolites”), varying in thickness from a few inches to
one or two feet. This bed is slightly developed between Manning-
tree and Harwich. At Dovercourt I have found remains of it with
its characteristic fossils on the top of the cliff; but it is in the
district between the rivers Orwell, Deben, and Alde that it is most
largely developed, and most profitably worked *. This bed often
has an underlie of large blocks of London-clay Septaria, and of
large, entire, and fresh-looking flints derived from the Chalk. In
this shingle are also found a considerable number of the larger shells
entire, particularly an abundance of Cardium edule, Pectunculus
glycymeris, Cyprina islandica, Trophon antiquum, &c., whilst the
Septaria are drilled by boring mollusks, and both Septaria and
flnts are covered with Balani. Large pebbles of siliceous sand-
stone, balls of concretionary dark fossiliferous sandstone, rolled and
worn bones or teeth of Cetacea, Sharks, &c., and occasionally frag-
ments of the older rocks, are also met with in this bed. Ata
pit at Trimley, near Felixstow, I found subangular fragments of
Lower Greensand chert, a large fragment of red granite, and frag-
ments and pebbles of siliceous sandstones. Although this shingle
and accompanying fragments of the older rocks are generally con-
fined to the base of the Red Crag, large blocks of angular flint and
seams of phosphatic nodules occasionally occur in the overlying beds.
Quartz pebbles are met with in the Red Crag, but they are rare.
This basement bed sometimes thins out +, and at other times
divides into two beds separated by a foot or two of shelly crag.
Sometimes also thin seams of phosphatic nodules occur 3 or 4 feet
above the lower bed, and separated from it by a bed of comminuted
shells, as at Foxhall, Waldringfield, and, in places, at Sutton. Di-
spersed nodules may, in fact, be found through the whole of the
Red Crag.
Above this basement bed are a series of beds more or less fossili-
ferous, forming with it the lower division of the Red Crag, which is
generally from 10 to 15 feet thick, and rarely attains a thickness of
from 20 to 25 feet. These beds are very irregular, not persistent
for long distances, often mere lenticular masses, and are marked
by the more or less constant occurrence of oblique lamination. This
lamination has not a constant direction. It varies to almost all
points of the compass. The dip is generally from 12° to 32°. A
common dip is about 22°, N.W., N.N.W., and N.E. It is in the
upper part of the lower division that false bedding is most general.
* Particularly in the district which surrounds the central mass of the Coral-
line Crag of Sutton.
+ In the cliff at Bawdsey this basement bed is altogether or almost wanting,
whereas half a mile inland it attains a thickness of from 2 to 3 feet.
PRESTWICH—-CRAG-BEDS OF SUFFOLK AND NORFOLK. 327
Sometimes the lower beds have been eroded previously to the de-
position of overlying beds, as in the following section at Ramsholt
(fig. 6).
Fig. 6.—Section in the Red Crag at Ramsholt.
SEE Ss = ZA SS
= = —SSS— Red Crag with few shells and
= = some coprolites, 10 feet.
=
——<——S
—————— SS
ec. Beam of coprolites.
tay Red Crag, 3 feet.
: Probable level of Coralline Crag.
In one instance only have I seen ripple-marks preserved in the
Red Crag. This occurred in the cliff at Bawdsey, where the argilla-
ceous lamin of one bed retained each a ripple-marked surface, which
in the section showed like the crumpled leaves of a book (fig. 7).
Figs. 7 & 8.—Sections in Bawdsey Cliff.
Fig. 7. Fig. 8.
Laminzx of ochreous clay and Bed of laminated clay and sand (4) with
of shelly sand. cracks at top filled with clay from a.
Another feature noticeable at times in the same cliff shows that
probably the shoals of the Red-Crag sea were occasionally left dry—
their surfaces fissured by the sun and air, and the cracks filled with
the materials of the bed afterwards thrown down upon them (fig. 8).
Elsewhere a crag-seam has been pressed down into an under-
lying bed, and the upper part afterwards removed as in fig. 9.
Fig. 9.—Section in Bawdsey Cliff.
= Ochreous clay.
Crag in hollows on top of
bed of grey clay with
seams of ironstone.
SS=SSHHSSSSSSSo5
SS— —— Crag.
ss = Ochreous clay.
The oxide of iron, to the presence of which the Red Crag owes
its distinctive name, is at places so abundant as to give rise to
; 2a2
328 PROCEEDINGS OF THE GEOLOGICAL SOCIBTY.
large tabular masses of very ferruginous sandstone and in places
to concretionary masses of limonite. Its introduction seems often
to have been subsequent to the formation of the beds. At some
places the same bed presents a stained and an unstained portion,
as in the following section* (fig. 10).
Fig. 10.— Section in the Cliff at Walton.
Red sand } 2
and crag.
=== | White sand
= | and crag.
The most remarkable result, however, arising from the presence ot
iron in these beds is exhibited in a pit near Butley Abbey (fig. 11).
Here the iron has segregated, not in distinct and separate seams
or nodules, but in large sections of the sands, throughout which it has
produced a pseudomorphous structure affecting the arrangement of
the beds themselves, which show on the one hand the concentric layers
due to the mineral action, and on the other the lamination due
to the bedding. The masses thus affected are as much as from
30 to 40 feet in horizontal diameter, whilst their vertical diameter
is but from 3 to 4 feet. The appearance at first sight is as if the
beds had been disturbed or reconstructed ; but a closer examination
shows that the lines of stratification extend through all the con-
centric ferruginous rings. Nevertheless the stratification is subor-
dinate to the action of segregation, which has so modified and
moulded the beds that the rings or, rather, coats of segregation, when
sufficiently consolidated, intersect the slightly consolidated sands and
grit just like planes of cleavage in the older rocks, and cause the de-
tached layers to peel off in accordance with the structure superin-
duced by the presence of the iron, and intersect the bedding at various
angles, These concentric rings pass indifferently through beds of
sand, grit, and crag, but are cut off sharply or are lost when they
come into contact with a seam more highly and entirely ferruginous.
It is the most illustrative instance of this kind of action of such
magnitude in beds of this class that has come within my knowledge.
From Walton to Aldborough the lower division of the Red Crag
abounds in shell-remains, the greater part comminuted, but with
many entire and single valves usually placed with their concave side
downwards. Some double shells, especially of Mytilus edulis, As-
tarte, Tellina, Mactra, and Corbula, occur, but they are not common.
With the exception of the old shore at Sutton, with its Mytil and
* Possibly the deep ferruginous colour of the Coralline Crag (g) at Sutton is
due to a staining received from encircling beds of Red Crag since removed.
CRAG-BEDS OF SUFFOLK AND NORFOLK. 329
PRESTWICH:
‘SpULd OLIjU9OUOD SHOULSNAL9F YPM SAI [BJUOZTAOY Podno]oo yysvy “G
“spoq-[[eyS “9 DF -QUOJSPULS-UOAT PUB GAD SNOUTSUALET LY @
‘evto snoeayoo A184 °G “SRL PAMMOIOO FYSVT *
{ AG LE [con geen “TL
“23 GS
= SSS ——
= ———— = —— =
—— = = = ——_ ———
—————— as === SS SS
—— ——_ —— = ==
—= ———— SS ee —s= SS = = = SSS
so Sas Se Ee ——— ee Z = — =
> = n= aaa =
a
: l
‘haqgy hang fo som apm v fypy ynogn uomUoyD 24] UO qT D UL wONIIG—TT “SI
330 PROCEEDINGS OF THE GEOLOGICAL SOCTETY.
Pholades, it would not be easy to fix upon a place in the Red Crag
where the Testacea are on the spot where they lived*. We meet
everywhere with finely comminuted shells and fragments of shells,
with here and there a band of more perfect specimens, or afew such
specimens dispersed amongst the comminuted fragments. Mr. Searles
Wood, however, considers that at Walton the conditions were such
that many of the Crag Testacea lived on that spot. Notwithstand-
ing the great number of shells occurring in the Red Crag, the
abounding and characteristic shells consist of a few species only,
and the larger proportion are more or less rare. Some species
occur in countless numbers, such as Cardium edule, Pectunculus
glycymeris, Tellina obliqua, T. crassa, T. pretenuis, Mytilus edulis,
Pecten opercularis, Maetra solida, M. arcuata, Cyprina islandica,
Lucina borealis, Purpura lapillus, Trophon antiquum, Nassa granu-
lata, NV. reticosa; while of many only a few specimens have been
found, and of some only one or two specimens. In places, especially
as we recede from the centre of the district, the beds become almost
devoid of shells, or they occur only in patches. This may be partly
owing to the original absence of shells, but it may also be due to
the removal of the shells by percolation of rain-water through the
beds ; for at places where the beds are consolidated by iron, casts of
shells are occasionally met with, as in some pits between Woodbridge
and Grundisburgh and elsewhere.
Mr. Searles Wood has given all the species he has procured from
the rich localities of Sutton, Walton}, Bawdsey, Foxhall, and New-
bourne. These localities are indicated by initials in the lists of Red-
and Norwich-Crag fossils; and therefore separate lists are not re-
quired. I have added some other localities.
Although some species are common throughout, there are many
which have only a limited distribution, and which give to various
localities their peculiar assemblages. This will be evident from the
general list at the end, as well as from the following local lists of
specimens, formed by me during occasional visits to the district.
From the pit near the Butley Oyster Inn.
Astarte Basterotii. Mya arenaria.
compressa. Mytilus edulis.
Omalii. Nucula Cobboldize.
Cardita senilis. nucleus.
Cardium angustatum. Pecten opercularis.
decorticatum. Saxicava arctica.
edule. Solen siliqua.
Corbula striata. Tellina crassa.
Cyprina islandica. lata.
Diplodonta astartea. — obliqua.
Loripes divaricata. preetenuis.
Mactyra ovalis. Dentalium costatum.
* Mr. A. Bell has obligingly given me a list of 54 species of Red-Crag shells
which he has found double. They are marked d in the general list.
+ See also Mr. Wood’s separate list from Walton in Quart. Journ. Geol. Soe.
vol. xxii. p. 542.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK.
Buccinum undatum.
Cancellaria costellifera.
Calyptrza chinensis.
Littorina littorea.
Natica.
Nassa granulata.
propinqua.
reticosa.
Purpura lapillus.
tetragona.
Ringicula buccinea.
Trophon antiquum.
costiferum.
gracile.
Trochus granulatus.
—— papillosus.
Turritella incrassata.
Voluta Lamberti.
Balanus crenatus.
331
The following is a list of shells furnished me by the late Dr.
Woodward, by whom they were collected at Chillesford Stack-pit
in 1863. The distance between the pits is one mile; and they are
both on the same level. Even in this short distance the distri-
bution shows a marked difference *. Some species rare or absent
in the last pit are common in this one :—
From the Chillesford Stack-pit.
Astarte Omalii. Tellina obliqua (common).
Cardium angustatum (common). pratenuis (common).
edule. Buccinum undatum.
Littorina littorea.
Natica catena.
clausa.
— wmultipunctata.
Purpura tetragona.
Trophon antiquum.
, var. contraria.
gracile.
Turritella incrassata.
venustum.
Mactra arcuata (common).
ovalis (common).
subtruncata.
Mya truncata.
Mytilus edulis.
Nucula Cobboldiz.
Pecten opercularis.
Pectunculus glycymeris (common).
Tellina crassa.
To these I may add—
Leda myalis. Nassa reticosa.
The following is also on the same authority :—
From a pit at Hollesley.
Cardium angustatum. Cerithium.
edule (frag.). Nassa granulata.
Mactra. —— reticosa (common).
Mya arenaria. Natica.
Pecten. Purpura lapillus.
Pectunculus glycymeris.
Tellina preetenuis (pair).
Buccinum tenerum.
Capulus ungaricus.
Trophon antiquum.
, Var. contraria.
gracile.
Turritella incrassata.
Between Chillesford and Aldborough a range of hills consisting of
a ridge of Coralline Crag, against both flanks of which the Red
Crag abuts, runs from Orford to Iken. On the eastern side of this
ridge there is on the whole a greater paucity of species. In one pit
* Telling, so very abundant generally in the Crag, do not occur at Walton,
or are at all events extremely rare.
332 PRODEEDINGS OF THE GEOLOGICAL SOCIETY.
the Red Crag may be seen capping the Coralline Crag; and I have
there collected the following fossils :—
Pit one mile east of Sudbourne Church.
Astarte obliquata. Tellina obliqua.
Cardium edule. Cyprzea europea.
Mactra ovalis. Littorina littorea.
Mya truncata. Nassa granulata.
Mytilus edulis. Purpura lapillus.
Pecten opercularis. Turritella incrassata.
To these a list of the late Dr. Woodward adds :—
Artemis lentiformis. Natica catena.
? Cardium Parkinsoni. ? Trochus zizyphinus.
Venus fasciata. Trophon antiquum*.
Buccinum undatum.
Proceeding northward there is a Crag pit, now little worked, just at
the back of Aldborough, in which the following fossils are found :—
Ballast-pit (near the gas-works), Aldborough.
Abra. Buccinum undatum.
Cardium edule. Littorina littorea.
Cyprina islandica. Purpura lapillus.
Lucina borealis. Trophon antiquum.
Mactra ovalis Turritella communis.
subtruncata.
Mya arenaria. Balanus crenatus.
Mytilus edulis.
Pecten opercularis. Large double shells of My-
Pectunculus glycymeris. tilus edulis are not un-
Tellina obliqua. common in this pit.
preetenuis.
A slight cutting on the railway one mile N. of Aldborough passes
through a thin bed of Red Crag with an abundance of Tellina,
Mactra, and Cardiwm. And in a cutting by the side of the road
to Saxmundham, on the hill one mile from Aldborough, Mr. Evans
and myself have collected the following species :—
Roadside one mile west of Aldborough.
Cardium edule. ? Clavatula linearis.
Leda myalis. Nassa.
Lucina borealis. Natica hemiclausa.
Mactra ovalis. Purpura lapillus.
Mya truncata. Scalaria clathratula (large).
Mytilus edulis. Turritella communis.
Pecten opercularis.
Tellina obliqua. Balanus crenatus.
preetenuis.
Calyptreea chinensis. Kehinocyamus pusillus.
In addition to these, Mr. Fisher mentions Bucconum undatum.
These few lists will serve to show the shells generally most com-
mon in the Suffolk Crag pits.
* Mentioned also by Mr. Fisher.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 333
The next pit northward is that on Aldringham Common (known
as the Thorpe Pit). As this, however, belongs to the so-called
Norwich Crag, we will proceed first to describe the upper divi-
sion of the Red Crag in the typical Sutton district, before com-
mencing with the district further north.
The upper division of the Red Crag I have formerly designated,
owing to the want of all fossils in the neighbourhood of Ipswich,
as the ‘unproductive sands”’ of the Red Crag ; but this, although it
holds good in the neighbourhood of Ipswich, cannot, if I am right in
its correlation, be applied as a general rule. Mr. Searles Wood,
jun., and Mr. Fisher, have also both noticed the presence of an
upper and more horizontally bedded division of the Red Crag, and
have remarked upon the difficulty at times of drawing a line of
separation between this and the underlying beds, owing to the
extent of erosion and denudation which had taken place immedi-
diately preceding the deposition of the upper bed*. There is great
difficulty (in many cases amounting almost to impossibility) in show-
ing where the line of separation really is placed. Where beds of
soft sand or loam are superimposed one upon the other, whatever
may be their difference of age, they must, when deposited under
water, tend to intermingle at the point of junction, as I have
shown in the case of the Loess in the neighbourhood of the
Reculvers, where it seems to pass gradually down into the Thanet
Sands. Therefore the apparent passage of two soft beds is unim-
portant when elsewhere a decided line of separation can be shown to
exist. Where the upper division of the Red Crag reposes quietly
upon the lower one, the similarity of lithological character and
colour is such that the only cause for separating them seems to be
the absence generally of organic remains in the upper division. But
this is not a persistent feature, as there are places where this division
contains shells, some of them of a marked character, to which we
shall refer presently +.
Some appearance of this upper division may be seen in the cliff at
Fig. 12.— Upper 25 feet of the Cliff, Walton-on-the-Naze.
LZZA Lie
a. Gravel. 3. Grey clay. 3’. Light coloured sand.
2. Crag beds. i. London clay.
* Ido not, however, interpret all the sections given by Mr. Wood (Ann. &
Mag. Nat. Hist. March 1864, pp. 3 & 4) in the same way that he does. I include
in the upper division of the Crag some beds which he considers to belong to his
“‘ Lower Drift.”
+ The line of division often shows best under certain conditions of weathering
and moisture.
304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Walton (fig. 12), where a bed of unproductive sands overlies the
shelly beds, and subtends them on to the London clay in a direction
from N. to 8.
In the railway-cutting between Woodbridge and Martlesham, this
upper division is more developed, and the lower division presents a
slightly eroded surface (fig. 13).
s. Fig. 13.—Section in Railway-cutting south of Woodbridge. yw.
{ =
=
a. White sand and gravel, 3 feet.
3'. Upper Red Crag, yellow sands with a few patches of shells at base, 15 feet.
2. Lower Red Crag, shelly, 12 feet. i. London Clay.
The erosion of the lower division now becomes marked both to
the eastward and northward of this place. Some well-marked 1-
stances may be seen in the cliff at Bawdsey (fig. 14), and again at
Shottisham (fig. 15).
Fig. 14.—Section in Bawdsey Chff.
Part of
upper
division ;
ochreous
sand with
few shells.
Z
ana ae :
Part of lower divison, with shells more numerous, and ferruginous.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 335
Fig. 15.—Section half a mile west of Shottisham Hall.
\
Upper division, with
ew Shells, 12 feét.
Shelly lower divi-
sion, 10 feet.
It is apparently this upper division of the Red Crag which reposes
on the eroded surface of the Coralline-Crag pit by the roadside
between Sudbourne and Iken (fig. 16).
Fig. 16.—Pit by side of road 1¢ mile N.N.E. from Sudbourne Church.
——— — == —— == == SS
=> SS == = S—= SSS — ——- SSS SS
—— —— = SSeS 2255
——
a. Light-coloured sands with fine gravel. _3'. Ferruginous and yellowsands. _1. Coralline Crag.
The same feature with relation to the Red Crag is again visible,
though not so clearly, at Aldborough (fig. 17).
Fig. 17.—Section in Ballast-pit, Aldborough.
——S—
(
|
|
|
The sandy beds of the upper division of the Red Crag do not
336 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
usually exceed from 10 to 15 feet in thickness, and pass upwards
into or are succeeded by the Chillesford Clay. This sequence is well
shown at Chillesford, where I had a trench dug in the upper pit
by the church down to the Red Crag, so connecting it with the
Stackyard pit. The general section thus taken is as under (fig. 18).
Fig. 18.—Section at Chillesford.
8. Light-coloured boulder-clay
with a seam of broken
sheil-fragments at base.
3. Grey clay with a few shells
and fish-vertebre, passing
down into light-coloured
: clayey sand, with patches
E = = = of perfect but friable
E ———————— shells.
Section in pit by side of
church
SSS =
: —— 3'. Yellow sands without shells.
a =>} == =
part proved == 2
by digging. =— The same with a few shells.
3 & 3’. Chillesford beds, 16 feet.
Seams of ferruginous sands
with a few seams of clay
and some shells.
— Se
Seams of comminuted
shells.
Pebbly sands.
Light-brown and iron sand,
with a greater variety
and more perfect shells.
Section in Stackyard pit.
Beds of comminuted shells,
with some entire ones.
2. Lower division of Red Orag, 22 feet.
—_——
The fossils of these Chillesford, or upper Red Crag, sands are often
very few; and some portion of them may in this district be derived
from the destruction of the lower division, in the same way that in
the lower division we find fossils derived from the Coralline Crag. At
Chillesford-Church pit, however, we get the fossils proper and pecu-
liar to these sands, as it is evidently the spot where they lived*. At
Walton a thin seam of undeterminable shell-fragments occurs in
places at the base of these sands. At Newbourne I could not di-
stinguish between the few fossils of these sands and those in the
beds beneath. At Chillesford Stack-pit Scrobicularia piperata is
stated by Mr. Searles Wood to be found in the upper part of the
* For lists of these fossils see Quart. Journ. Geol. Soc. vol. v. p. 350, and
vol. xxii. p. 545; also the general list.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 337
section in association with other shells of the Chillesford series, such
as Oyprina islandica, Mactra ovalis, Mya truncata, Tellina obliqua
T. lata, and T. pretenuis, in sands resting upon beds of the Re
Crag.
I have collected in these upper beds at Bawdsey cliff :—
Astarte compressa. Buccinum undatum.
Cardita scalaris. Littorina littorea.
Cardium edule. Nassa reticosa.
Cyprina islandica. Natica catena.
Lucina borealis ? hemiclausa.
Mactra solida. Trophon antiquum, var. con-
Mya arenaria. traria.
Mytilus edulis. Turritella communis.
Pecten opercularis.
Pectunculus glycymeris. Sphenotrochus intermedius.
Tellina obliqua. Vertebrz of fish.
preetenuis. Teeth of shark.
Nucula Cobboldiz. Claws of crab.
Owing to the presence of derived fossils, and the similarity of
lithological characters of this division in the Red-Crag district
proper, it will require special and careful search to determine its
fauna in this area. Most of the shells are probably im common ; but
the variation in physical conditions, independently of other circum-
stances, will be found, no doubt, to have brought in fresh species.
Fig. 19.—Section in Chillesford brick-pit.
Boulder-clay.
| chiestora clay with
impressions of shells.
Chillesford sand re-
posing on Red Crag.
These sands are succeeded by laminated grey clays, the lower parts
of which are seen at Chillesford-Church pit, but are better developed
at Chillesford brick-pit. The clay is there fossiliferous ; but the shells
are all in the state of casts and impressions in the clay. The fol-
lowing species are recognizable :—
Arca. Leda myalis.
Cardium greenlandicum. Nucula tenuis.
Cyprina islandica. Tellina lata.
338 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
I had always been told that large bones were occasionally found
in these clays; but it was not until this last winter that any were
brought to my notice, when I was informed that the bones of some
large animal had been discovered; and on visiting the pit in com-
pany with Mr. Gwyn Jeffreys, I was shown the vertebral column of
a great whale at a depth of 8 feet from the surface, and lying at
right angles to the face of the section. These vertebrae were exactly
in the position in which they might have been left at the death
of the animal—each vertebra lying a few inches apart from its
neighbours, owing to the removal of the cartilaginous matter be-
tween them. About seven vertebre have been taken out; and it
is to be hoped that a further portion of the skeleton may yet be dis-
covered *. Fig. 19 is a sketch of this pit.
As this clay forms an important link in the correlation of the
Suffolk with the Norfolk Crags, I will, before touching upon the
latter, proceed to trace it from south to north through the Red-Crag
area.
Commencing at the furthest point south, the bed of clay (see
fig. 12, bed 3) overlying the sands at Walton-on-the-Naze should
probably be referred to this zone. In mineral character it
closely resembles the Chillesford clay ; and it contains in places, as
it does again further north, fragments and pieces of wood, but I
could here find no traces of shells. In the Ipswich and Woodbridge
districts this clay is not seen, and the gravels of the Boulder-clay
series repose immediately upon unproductive Chillesford sands or on
the Crag. The clay is met with on the hills in the neighbourhood
of Felixstow, and again near Hollesley; but it is at Chillesford
that it is best developed and becomes fossiliferous. It may be
traced capping the hills between Sudbourne and Iken. Some
time since, there was a good section in a pit half a mile north
of Black Walks, in the direction of Iken. A laminated clay, 8 or
10 feet thick and full of the casts of the following shells, there
overlies a bed of light-coloured sands, under which, at a depth of
a few feet, the Red Crag was reached in a trench I had dug :-—
Cardium greenlandicum. Nucula tenuis.
Leda myalis. Tellina lata.
And in the same clay at the pit at Low Farm we found :—
Cardium greenlandicum. Scobicularia piperata.
Leda myalis. Turritella communis.
Nucula Cobboldiz.
There was formerly a pit on Webber’s Whin Farm, a mile and a
half W.S.W. from Aldborough Ferry, where the fossiliferous Chilles-
ford sands occurred, and with them a group of shells to which
elsewhere special attention has been directed by Mr. Fisher, by
whom this bed has been termed the Mya-bed, from the abundance
* Dr. Crisp has since ascertained it to be an entire whale 31 feet long. (Brit.
Assoc. Rep. 1868, Trans. Sect. p. 61.)
t+ “On the Relation of the Norwich Crag to the Chillesford Clay or Loam ”
(Quart. Journ. Geol. Soc. vol. xxii. p. 19).
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 309
of that shell in it. When I again visited it lately to collect more
of the fossils, I found it sloped over.
The clay contained numerous impressions of the same shells as at
Iken, and in the same condition ; but in the sand the shells them-
selves were preserved, mostly double and in the position in which they
lived. They consisted of :—
Cardium. Nucula or Leda.
Mya truncata. Tellina.
Crossing the Alde, the hill at the back of Aldborough is capped
by the Chillesford clay, with the sands under it, and we again find
it at the brick-pit near Warren House, one mile N. of Aldborough;
but in neither of these places have I found any fossils. Their relation
at the latter place, both to the Red Crag and Coralline Crag, is clear,
as shown in the following theoretical section :—
Fig. 20.—Section from the Railway to the High-road, near
Warren House: height about 25 feet.
cutting.
Railway-
a. White sands and gravel. 2. Red Crag.
3. Chillesford Clay. 1. Coralline Crag.
3’. Chillesford Sand.
The shell-bed on the side of the road to Saxmundham shows
also, apparently, the same relation to the-Chillesford Clay, if we
may Judge by a bed of clay which crops out near the top of the hill.
These Chillesford clays form with the underlying sands the upper
division of the Red Crag.
Before leaving this district, I must direct attention to some sec-
tions of much interest, both on the score of old physical geography
and in evidence of the dependent relations of the Red to the Coral-
line Crag. To the first of these sections attention was originally di-
rected by Sir Charles Lyell in 1838. In his description of the Crag
at Sutton, Sir Charles pointed out that in the Bullock-yard pit on Mr.
Colchester’s farm the Red Crag abuts against the Coralline Crag,
and that the latter is perforated by Pholades, showing the existence
of an old cliff, and that this cliff was subsequently submerged and
covered up with Red Crag. ‘The further opening out of this section
and some other sections on the opposite side of the hill show that
there are two submerged cliffs, that they pass round the hill, and that
the mass of Coralline Crag, forming the higher part of the hill, has
been an old reef in the Red-Crag sea. We have additional evidence
also showing how great was the denudation and removal of the
Coralline Crag, the débris of which is profusely scattered in some
adjacent beds of the Red Crag. The facts were of so much interest
that I resolved to have a properly levelled section taken of the whole
340 PROCERDINGS OF THE GEOLOGICAL SOCIETY.
ground; and for that purpose I applied to Mr. P. Bruff, C.K., of
Ipswich. This gentleman very kindly offered me the gratuitous
services of his assistant, Mr. Miller, to run a level from the river
Deben to Shottisham ; and I am indebted to him for the careful levels
and plan given in Pl. VI.
This survey has furnished the data for my section at Sutton, where
the old cliffs and shore-lines are shown (map and sections, Pl. VI.),
Fig. 21.—Section in Bullock-yard jit, Sutton (D, Pl. VI.).
Red Crag.
s'. Upper shore-line, with
blocks of Coralline Crag,
s' flints, coprolites, and
shells.
Coralline Crag.
s’. Lower shore-line, with
a seam of Mytili (m) and
® a bed of coprolites (7).
Fig. 22.—Section im the same pit, but at right angles to the above.
= Eo = = FT
SSS Red Crag with two
(= Ss. boulders of Coralline Crag,
ZAC showing that No. 1 fell
== before, and No. 2 after the
deposition of bed r.
Red Crag with nume-
rous blocks and fragments
of Coralline Crag, show-
ing the section of the lower
shore on W. side of the
reef.
while the details of them as seen in two of the pits are given in
figs. 21, 22, and 23. The upper shore-line s! is 31 feet above high
PRESTWICH—-CRAG-BEDS OF SUFFOLK AND NORFOLK. 341
water of the river Deben, which can vary but little from that of
the sea on the adjacent coast, from which this part of the river is
only five miles distant. The upper cliff (0’, fig. 21), which is not
well exposed, is about 12 feet high, and must formerly have been
higher, as blocks of the consolidated bed of Bryozoa capping the
hill higher up are found at its base. They may have toppled over
the brow of the old cliff, or been detached and carried a short dis-
tance by ice-action. At all events it is evident, from the way in
which the blocks of Coralline Crag, 1, 2 in fig. 22, have impressed
and squeezed up the lower layers of Red Crag in which they rest,
that they fell on the spot where they now lie whilst the Red Crag
was in course of formation, and that the upper part of the Red
Crag was deposited subsequently to the fall of the blocks. The
larger of these angular blocks of Coralline Crag may weigh more
than a ton. In addition to these large blocks there are many
smaller ones—some perforated by Annelids, and others covered with
Balani (B. crenatus). Together with these are a number of pebbles
of flint, some coprolites, and some large masses of angular and un-
worn flints. Interspersed with this coarse shingle are an abundance
of shells (chiefly Mytilus edulis) with both valves. The Pholas-
perforations commence at the top of the upper shore, and pass over
the brow of the lower cliff, 0. A few feet back from the face of the
section the Coralline Crag rises to the surface of the ground.
To ascertain the position of the lower shore-line, I had a trench
dug at the bottom of the pit and below the level of the upper shore,
s' (fig. 21). I found the Red Crag to extend about 4 feet deeper,
and at its base a shingle composed of phosphatic nodules and of
large flints, over which there was a thin bed of Mytilus edulis, almost
all with the two valves, and apparently in the spot where they lived.
This shore-line is 22 feet above high-water mark. Its character
is better seen in a pit (G) situated on the other side of the old reef,
350 yards west of the pit D (see Pl. VI.). The details of this pit are
given in fig. 23. On the upper shore in pit D I found only two large
blocks of CorallineCrag ; but onthis lower shore the blocks were many,
whilst numerous smaller fragments were dispersed throughout the
section, showing the removal of the adjacent Coralline Crag to have
been more active at the commencement of than further on in the
Red Crag period. Flints and phosphatic nodules are dispersed here
and there. Apparently this pit is at a rather greater distance than
pit D from the old submerged reef.
The occurrence of these transported blocks of Coralline Crag is
peculiar to these pits. There are, however, few other pits so near as
these to the Coralline Crag ; and the upper bed of the Coralline Crag
is here also more compact thanelsewhere. But although the débris
of the Coralline Crag is nowhere else so abundant, it may never-
theless be detected in most of the pits of the Red Crag in this dis-
trict. Small pieces and fragments of the harder seams of the Coral-
line Crag, together with its Corals and Bryozoa, are extremely common
in the Red Crag at Waldringfield, one mile direct from Sutton. I have
also found worn fragments of the Coralline Crag in the Red Crag at
VOL, XXVII,—PART I. 2B
Red Crag.
12 feet.
Coralline
rag.
8 feet.
342 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Bawdsey and Felixstow. Flat pieces of the thin limestone seams __
of the Coralline Crag are common in the Red Crag around Tatting-
stone, where the same reef-like structure of the Coralline Crag is
shown at Park Farm (fig. 24); and I have found some small frag-
ments even in the Red Crag at Walton.
Fig. 24.—Pit at Park Farm, Tattingstone, near Ipswich.
White sand.
Another old Coralline-Crag reef forms the nucleus of the ridge of
hills from Gedgrave and Orford to Iken and Aldborough. ‘The Red
Crag abuts against its flanks, and its summit is capped by the
Chillesford clay ; but although the Red Crag can be traced close up
to these hills, the cliff-line is nowhere exposed. At the same time
the erosion of the Coralline Crag adjacent to this old reef during the
Red-Crag period is seen in the section given in fig. 15. It is pro-
bably the littoral zone of an old shore connected with a higher part
of this reef or islet that is indicated by the Mya-bed of Mr. Fisher.
Having described the Red Crag and Chillesford series in their
typical and special area, and followed them as far as Aldborough, we
come to more debatable ground. Some geologists have referred the
crag at the Aldborough ballast-pit to the Norwich Crag, and others
to the Red Crag. The next sections, however, which are only two
miles further north, present far more definite characters. Their re-
lation to the Norwich type cannot be doubted ; and to that group they
have always beenreferred. It remains now to be seen whether there
are sufficient grounds for considering the Crag in the area north of
Aldborough to be newer than the Red-Crag series, or whether it is
to be considered a synchronous deposit, with differences of character
depending upon local conditions.
We have already noticed three ridges of Coralline Crag—one at
Tattingstone, a second at Sutton, and a third extending from south
of Orford to Iken and Aldborough. The first two are small, and
the Red Crag wraps round them without any change of character.
The third is more important and makes a greater break in the Red
Crag, which nevertheless reappears on its eastern flank, although
Crag with a ew ¢
prolites.
Brown loam.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 343
with characters somewhat modified. The Coralline-Crag ridge ap-
pears to be further prolonged from Aldborough nearly to Sizewell ;
and it is on the northern side of this that we find the marked change
in the newer Crag. From this point the characteristic land and fresh-
water features of the Norwich beds set in, and the typical Red Crag
is no longer met with.
Let us therefore see what relation the more northern Crag bears
to the Chillesford Clay, and in what the difference in organic remains
from the Red Crag consists.
The cliff at Thorpe is now overgrown; but the Boulder-clay
appears in pits a short distance inland. At Sizewell traces of crag
may be seen in the cliff; and a few years since the digging of a
well * brought to light additional specimens, of which I collected :—
Fossils from Sizewell Cliff.
Astarte compressa.
Cardium edule.
—— interruptum.
Cyprina islandica.
Lucina borealis.
Mactra ovalis.
Mya arenaria.
Mytilus edulis.
Nucula Cobboldiz.
Tellina obliqua.
— lata.
preetenuis.
Cerithium tricinctum.
Conoyulus pyramidalis.
Nassa inerassata.
Natica hemiclausa.
Paludina lenta.
Purpura lapillus.
Trochus Kicksii.
Turritella communis.
Base of horn of deer, in pre-
cisely the same condition as
Red-Crag specimen.
together with fragments of Coralline Crag drilled by boring-shells
and Annelids and covered with Balani.
A mile and a half W.S.W. from Sizewell is the well-known pit
on Aldringham common, generally known as Thorpe pit. Here,
again, no superposition is seen. The Boulder-clay caps the hill
between this pit and Sizewell ; and the Chillesford Clay appears on
higher ground to the westward. At Sizewell the crag is more or
less ferruginous, like the Red Crag ; but here it is light-coloured, like
the Norwich Crag. The following is a list of the shells that my
friend Mr. Evans and I have collected there on various occasions :—
Tast of Fossils from Thorpe pit, near Aldborough.
Abra obovalis ?
Astarte gracilis.
Cardium edule.
Corbula striata.
Cyprina islandica.
Donax trunculus.
Lucina borealis.
Mactra ovalis.
Mya arenaria.
Mytilus edulis.
Pecten opercularis.
Pectunculus glycymeris.
Solen siliqua.
TYellina lata.
Tellina obliqua.
preetenuis.
Buccinum undatum.
Cerithium tricinctum.
Calyptrxa chinensis.
Conovulus pyramidalis.
Littorina littorea.
Natica.
Paludina lenta.
Purpura lapillus.
Scalaria greenlandica.
Trophon antiquum.
Turritella communis.
incrassata.
* There was 20 feet of unpreductive sands above the shell-bed.
D5 2
344 PROCEEDINGS OF THR GEOLOGICAL SOCIETY.
Platax Woodwardii.
Raia antiqua.
Balanus crenatus.
Claw of crab.
Vertebre of fish.
Some undeterminable mammalian bones and fragments of deers’
horn have also been found by Mr. Evans.
The next pit to the north is at Bulchamp, near Wangford, ten
miles distant, the intervening country presenting, as usual, low hills
of Boulder-clay and unproductive sands. Some years since, a section
nearly 20 feet deep was well exposed (fig. 25) ; now little is to be seen.
Fig. 25.—Pit near Bulchamp Union.
S555 Hs —=— ——=
Zz
In appearance and colour the pitis precisely like a Red-Crag pit ;
and it will be observed that we have here a repetition of the marks
of erosion which we have noticed between the two divisions of the
Red Crag in the Sutton district ; or it may only be an eroded shoal
in the lower division, as at Ramsholt (fig. 6). The shells I have
found there are as under :—
List of Fossils from Bulchamp-pits of the Union. (See also the
general list.)
Abra alba.
Actzon Nos.
Astarte.
Cardium edule.
Corbula nucleus.
Cyprina islandica.
Leda myalis.
Mactra ovalis.
subtruncata.
Mya arenaria.
—— truncata.
Mytilus edulis.
? Panopeea norvegica.
Tellina lata.
obliqua.
pretenuis.
Scrobicularia piperata.
Buccinum undatum.
Cerithium tricinctum.
Conovulus pyramidalis.
Bulimus.
Littorina littorea.
Natica catena.
Paludina lenta.
Purpura lapillus.
Trophon antiquum.
Turritella communis.
Scalaria greenlandica.
Balanus crenatus.
Claw of crab.
Vertebree of fish.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 345
The level of this pit is very little above that of the river. There
is no superposition with any other bed; but I consider there are indi-
cations of the Chillesford Clay on higher ground between it and
Wangford.
There is another pit one mile south of Wangford, again without
superposition and but little above the level of the river. It presents
very similar features to the pit on Thorpe common, the beds being
light-coloured and pebbly. The common shells are Cardiwm edule,
Mya arenaria, Littorina littorea, Purpura lapillus, and a few others.
Passing thence to the N.E., we find in the cliff at Easton Bavent,
from one to two miles north of Southwold, a section of much interest,
as it shows distinctly the relation of the Chillesford Clay to the so-
called Mammaliferous or Norwich Crag. The section some years since
was remarkably clear, and presented the following features (fig. 26).
Fig. 26.—Cliff at Easton Bavent.
a. Light-coloured sand and shingle.
3. Grey laminated clay, 4 to 6 feet.
3 3, Sand, pebbles and shells, 3 feet.
Along part of the cliff I found no organic remains in the clay; but
at the more northern end of the cliff I met with them at one
spot in considerable abundance—many with double valves and in
the position in which they lived. Leda myalis was common. The
following is a list made on a first and on a subsequent visit with
Mr. Jeffreys :-—
Fossils from the Chillesford Clay (8, fig. 26), Haston Bavent.
Astarte compressa. Tellina lata.
Cardita scalaris. — obliqua.
Cardium edule. —
Corbula. Buccinum undatum.
Cyprina islandica. Littorina littorea.
Leda myalis. Natica cirriformis.
Lucina borealis. Purpura lapillus.
Mactra ovalis. Turritella communis.
subtruncata.
Mytilus edulis. One leaf-impression.
Nucula Cobboldiz.
while in the pebbly sands which here underlie the Chillesford Clay,
sometimes in immediate contact with it, and at other times separated
by 2 or 3 feet of light-coloured sand, we have found :—
Fossils from the Crag Bed (3', fig. 26), Easton Bavent (Southwold).
(See also the general list.)
Abra obovalis. Astarte borealis.
Avytemis lincta. compressa.
346 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Cardium edule.
Circe minima.
Corbula striata.
Cyprina islandica.
Leda myalis.
Lucina borealis.
Mactvra ovalis.
subtruncata,
Mya arenaria.
Mytilus edulis.
Nucula Cobboldize.
Tellina lata.
obliqua.
pretenuis.
Buccinum tenerum.
undatum.
Conoyulus pyramidalis.
Littorina littorea.
Natica catena.
Purpura lapillus.
Trophon antiquum.
Turritella communis.
Pecten opercularis. Balanus crenatus.
There are also here found remains of
Platax Woodwardii. Raia antiqua.
Vertebre of fish. Balzena vertebree.
Mastodon teeth.
In the Museum of the Geological Society there is, amongst the
specimens presented by Capt. Alexander, a rolled Coralline-Crag
‘coral from Southwold.
There are pits at Henham and Yarn Hill, to the N.N.W. of South-
wold, which yield a similar but poorer group of fossils from sand-
beds which are also below the Chillesford Clay.
Fossils from Yarn Hill (including Mr. Fisher's list*).
Astarte borealis. Cerithium tricinctum.
Cardium edule. Littorina littorea.
Cyprina islandica. Natica catena.
Mactra subtruncata. Guillemini.
ovalis. Paludina lenta.
Pinna, Purpura lapillus.
Tellina obliqua. Ringicula buccinea.
—- lata. Succinea oblonga.
preetenuis. Trophon antiquum.
This completes the series of the Crag-pits in Suffolk. Those of
Norfolk will be described in the next part of this paper.
OrGAnic REMAINS.
It is evident that the organic remains of the Red Crag must be
divided into two categories—the one of fossils proper to the forma-
tion, and the other of fossils derived from other formations. Generally
the extraneous fossils of any deposit are few; but in the case of the
Red Crag they constitute a very important section and require a careful
elimination. Mr. Searles Wood communicated a paper to the Geo-
logical Society in 18597, in which he expressed an opinion that:—
3 Bisice: Cintinodia were possibly derived from the Co-
8 . Zoophytes ralline Crag.
* Quart. Journ. Geol. Soc. vol. xxii. p. 26.
t “On the Extraneous Fossils of the Red Crag,” by 8. V. Wood, Esq., F.G.S.
(Quart. Journ. Geol. Soc. vol. xv. p. 32).
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 347
12 species of terrestrial Mammalia
AS Cetacea |
es Ziphioid Cetaceans probably derived from Upper Ter-
Fish - tiaries.
as Testacea >
‘i Mammalia
x Fish |
Mammalia \
i
probably derived from Middle Ter-
tiaries.
o Reptiles
Fe Fish
Testacea
Crustacea
Echinoderms
x Zoophytes )
Of the origin of the fossils from the older Tertiaries (London Clay)
there can be no doubt, as they are well-known species of that for-
mation, and have the mineral condition proper to it. The number
of Crustacea and of Fishes derived from that source could now be
even largely increased.
With regard to the origin of the mammalian remains, Mr. Searles
Wood expresses an opinion that the land-mammalia “ are certainly
intruders into the Crag, to whatever period they may be assigned.”
In his paper on the extraneous fossils of the Red Crag, he considers
some of them to be of Middle-Tertiary age, but that the majority
belong to the Upper Tertiaries, and are of older date than the Red
Crag. He also suggests the questions whether the large fish-teeth
from Suffolk may not be from beds of the same Miocene age as
those of Malta; and he raises the same question with regard to
the remains of Hippotherium and Hyenodon.
In 1840, in 1846, and lastly in 1856, Professor Owen * described
various mammalian fossils of the Red Crag ; and he came to the con-
clusion “ that the majority of them are identical or closely correspond
with the Miocene forms of Mammalia, and especially with those from
the Eppelsheim locality described by Professor Kaup. In Suffolk,
as in Darmstadt, we find Mastodon longirostris (angustidens), Rhi-
noceros Schleiermacheri, Tapirus priscus, Sus palewocherus, and Cervus
dicranocerus associated together in the same formation; and with
these Miocene forms of extinct Mammalia in the Red Crag we have
likewise the Cetaceans, which most closely resemble the Miocene
species of that order previously recognized in the Crag or Molasse of
the Continent.”
In 1857, Dr. Falconer published an important paper on the spe-
cies of Mastodon and Elephant occurring in a fossil state in Great
Britain. To this paper are appended some interesting remarks on
other mammalian fossils of the crag. He established the identity
of the Crag-Mastodon with the M. arvernensis of Auvergne and
Velay. With regard to the Crag-Rhinoceros, he considered that the
teeth present no character, so far as they have been described, incon-
sistent with their being referred to the so-called 2. megarhinus of the
bo ho
RBbWoOrROPOIMOONK
probably derived from older Ter-
tiaries.
* Ann. & Mag. Nat. Hist. vol. iv., ‘British Fossil Mammalia,’ and Quart.
Journ. Geol. Soe. vol. xii. p. 217.
t Quart. Journ. Geol. Soc. vol. xi. pp. 347-360.
348 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
south of France and Italy. After reviewing the other species of
Mammalia, he states that ‘ they agree generally, as far as the species
have been well determined, with the great Pliocene fauna of Italy,
as exhibited along the valleys of the Po and Arno; but it must, at
the same time, be freely admitted that the materials upon which the
determination of many of the species of the Red-Crag Mammalia at
present rests are so scanty and undecisive that the identification
either way, whether as Miocene or Pliocene forms, must be regarded
as little more than approximate.” He proceeds to say :—
“‘There are other considerations which corroborate the Pliocene
view of the mammalian fauna of the Crag. The debatable species
referred by Professor Owen to Miocene origin all belong to genera
that are common to the Miocene and Pliocene periods, such as
Mastodon, Rhinoceros, Tapirus, Sus, Cervus, and Felis; but of the
more remarkable types which are limited to the Upper Miocene de-
posits, and which abound in them all over Europe, such as the Dino-
therium, Chalicotheriwm, Aceratherium, Anchitherium, Amphicyon,
&e., not a single remain has ever been eited as having been found
in the Crag-deposits. The question naturally arises, how does it
happen, if the majority of the Red-Crag Mammalia are Miocene, that
there has been this selective admixture of species of long-termed
‘Miocene’ genera in the Crag, and why the exclusion of the strictly
characteristic genera ?”
Professor Huxley, in a paper* on the Cetacean fossils termed
Ziphius by Cuvier, read before this Society in 1864, shows the rela-
tion of the Suffolk fossils to those of the Antwerp Crag.
Mr. Ray Lankester +, in a communication to the Society in 1865,
described some interesting new fossils from the Red Crag, and, in
speaking of the sources of the mammalian fossils of the Red Crag,
also states, “as an extension or modification of the views which had
been formerly advanced, chiefly by Mr. Searles Wood,” his econclu-
sion that the mammalian remains of the Red Crag are mostly derived
from earlier beds—“ the Ziphioid Cetaceans (with Carcharodon &c.)
from an equivalent of the Middle Antwerp Crag—the Mastodon,
Rhinoceros, Tapir, Sus, Felis, &c. perhaps from a late Miocene, or
more probably from an earlier Pliocene bed”.
* Quart. Journ. Geol. Soe. vol. xx. p. 388. + Zoid. vol. xxi. p. 221.
{ The recent papers of Prof. Owen (Pal. Soc. 1869) and of Mr. Ray
Lankester (Quart. Journ. Geol. Soc. Nov. 1870) enable us now to give a more
complete and correct list of the Vertebrate remains found in the Red Crag :—
Lanp. Marine.
Castor veterior, Lank. Baleznodon afifinis, Ow.
Cervus dicranoceros, Kaup. —— definita, Ow.
Equus placidens ?, Ow. —— emarginata, Ow.
Felis paroides, Ow: —— gibbosa, Ow.
Hipparion. —— physaloides, Ow.
Hyeena antiqua, Lank. Belemnoziphius compressus, Hux.
Mastodon arvernensis, Cr. ¢ Jo. Carcharodon megalodon, 4g. —
—— (tapiroides?, Cuv.). Choneziphius Packardi, Lank.
Rhinoceros Schleiermacheri, Kaup. —— planirostris, Lank.
Sus antiquus?, Kaup. Delphinus. :
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 349
While, therefore, all agree in considering the mammalian remains
generally to be extraneous fossils, there is a difference of opinion,
but not a great one, with respect to their age and origin. Some
small portion of these fossils are doubtless of the age of the Red
Crag. Unlike the great proportion of the Mammalian and Ceta-
cean remains, which possess so peculiar a fossilization, are so dense
and so worn that they show at once their extraneous origin, some of
the large Whale-vertebree and some of the small fish-vertebre are
so little mineralized and worn that they cannot be considered de-
rived fossils*. At the same time the very circumstance that a
portion of the Cetacean remains are, like the land Mammalian re-
mains, heavily mineralized and worn, makes one cautious how far
that mineralization and that wear should be construed as a proof of
extraneous origin.
The discovery by Mr. Colchester (ante, p. 117), in the pit which
he opened at Sutton, of teeth of Mastodon, Rhinoceros, &c., with
Cetacean remains, all of the same species as those found in the Red
Crag, and, like the latter, im a shingle-bed at the very base of
the Coralline Crag, shows that some of these remains of the Red Crag
may have been derived directly from the Coralline Crag, although
they may have to be carried yet further back in the geological series +;
while I consider it probable that some will be found to be of the
age of the Coralline Crag itself.
Mr. Darwin describes t eight species of Cirripedia from the
Red Crag, of which six are living and two supposed to be extinct.
Edward Forbes § described six species of Echinoderms, one of
which only he identified with a living species; but one is proba-
bly derived from the Coralline Crag ; Hchinocyamus suffolcensis is
probably only a variety of the H. pusillus; and Kchinus Henslowit
he thought might be related to an undescribed species from Iceland.
This would give one extinct to three living species.
Lanp. Marine.
Tapirus priscus, Kaup. Lamna.
Ursus arvernensis, Cr. § Job. Otodus.
Megaceros hibernicus ? Phoceena.
Squalodon (antverpiensis ?).
To these I would add Trichecodon Huxleyi, Lank.
EHlephas (meridionalis ?). Ziphius angulatus, Ow.
—— angustatus, Ow.
— compressus, Ow.
gibbus, Ow.
—— medilineatus, Ow.
—— planus, Ow.
—— tenuirostris, Ow.
* The finest series of the extraneous fossils of Red Crag I know of is that form-
ing part of the valuable collection of Red-Crag fossils in the possession of Mr.
Whincopp, of Woodbridge, who has devoted much time and care to secure the
many rare specimens brought to light by the Coprolite-diggings which for the
last few years have been carried on so actively in the neighbourhood of Sutton
and Woodbridge.
+ In the same way it is probable that the dark sandstone nodules, with casts
and impressions of shells, so common in the Red Crag at Bawdsey, Sutton,
&c., may have been derived indirectly through the Coralline Crag.
+ Pal. Soc. 1854. § Lhid. 1852.
300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
The four Corals, the Bryozoa, and the Foraminifera found in the
Red Crag must be looked upon with doubt in presence of its richer
neighbour the Coralline Crag, which has evidently contributed so
largely to its stock*.
Mollusca.—Mr. Searles Wood describes in his monograph 239
species of shells. Of these he considers that 53 species are pro-
bably derived from the Coralline Crag, leaving 176 proper to the Red
Crag+. A certain number of these latter were formerly considered
to be extinct species; but the important researches in deep-sea
dredging carried on of late years by Mr. Gwyn Jeffreys and others have
shown that many of the species formerly supposed to be extinet
still exist in the deeper parts of the Atlantic and Mediterranean.
Many species, also, which were considered to be distinct are now
regarded as varieties.
With a view to the modifications in the relations of the Red-Crag
fauna to the recent one which these changes render necessary,
Mr. Jeffreys has kindly gone through the list I had tabulated from
Mr. Wood’s monograph, added some new species, eliminated the
varieties, and identified the species found to be now living.
On the question of the species which are to be considered ex-
traneous, there is still considerable difference of opinion. Mr. Jef-
freys justly states that “the question of which species may be
extraneous or derivative is at present in an unsatisfactory state.”
It is a difficulty which has been felt by all observers, from Mr.
Charlesworth to Mr. Wood. For my own part I should be almost
disposed to regard the greater number of the species found in the
Crag of Suffolk and not in the Crag of Norfolk as derived from the
Coralline Crag. So large a proportion of the latter has been de-
stroyed, and, as it were, incorporated into the Red Crag, that I can
conceive even certain species of the older deposit being now found
only in the newer one. It would, however, be too much to assume
such an origin for so large-a proportion of these fossils.. In the fol-
lowing list I have considered the fact of any species being found also
in the Norwich Crag a sufficient reason for removing it from the
list of extraneous fossils. As a rule I have also regarded the species
found at Walton{, together with those occurring in the Sables
* Prof. Duncan has recently described (Geol. Soc. April 1871) a new coral
from the Red Crag of Waldringfield, which he has named Solenastrea Prest-
wichit.
+ Mx. Wood now reduces the number of extraneous shells to 25; and Sir
Charles Lyell reestimates the extinct species as under :—
Percentage of
Total Number. Nownere shells not
Be pnures known as living.
Bivalves .......cece00c8 128 31
Univalves ............ 127 33 | 25
Brachiopods ......... 1 1
(See ‘Student’s Elements,’ p. 178.)
{ The circumstance even of a fossil occurring at Walton does not exclude the
possibility of extraneous derivation; for I have found fragments of thin lime-
stone from the Coralline Crag even there.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 301
jaunes of Antwerp and not in the Sables gris, with such species as
survived to the glacial period in England, as species proper to the
Red Crag. I doubt whether the circumstance of a shell being found
double in the Red Crag is sufficient to identify it with that deposit,
as, from the compactness of portions of the Coralline Crag, I see no
reason why many should not have been transferred from one to the
other without break.
Species probably derwed from the Coralline Crag.
Terebratula grandis. Caneellaria mitreeformis.
Astarte Burtini. Chemnitzia costaria.
Basterotii. Conopleura Maravigne.
—— mutabilis. Dentalium costatum.
Cardita senilis. Erato Maugerie.
Cardium decorticatum. Nassa labiosa.
Chama gryphoides. —— prismatica.
Cyprina rustica. ? Natica varians.
Diplodonta dilatata. Odostomia plicata.
? rotundata. Pleurotoma carinata.
Donax politus. semicolon.
Erycinella ovalis. Pyrula acclinis.
Gastrocheena dubia. Rissoa costulata.
Hinnites Cortesyi. Scalaria foliacea.
Leuconopsis Lajonkaireana. fimbriosa.
Limopsis aurita. varicosa.
Ostrea princeps. Terebra inversa.
? Panopeea Faujasii. canalis.
plicata. Trochus Kicksii.
Pecten dubius. villicus.
Pholadidea papyracea. Trophon alveolatum.
Venus ovata. consociale.
Cecum mammillatum. Vermetus intortus.
I feel that much uncertainty must still attach to such a list ; and
Y may remark that Mr. Jeffreys takes the lesser number of 13 species
as derived.
Allowing for this element, the result is that the species found in
the Red Crag are as under :—
Number according to Mr. Wo0d’s list .........eessseeeeeeseneees 239
New species added by Mr. Jeffreys and Mr. Bell............... i
Species regarded by Mr. Jeffreys as varieties.............06-.-00-
Species for the first time identified as recent by Mr. Jeffreys 46
HEX EAT EO US'S PCCLOS.s.enepes ss atria see aeons eosct ose ecene ses ees 46?
Excluding the varieties and extraneous species, this leaves as
proper to the Red Crag 234 species, composed as under :—
Total Living Extinct Proportion of
species. species. species. extinct species.
234 216 18 7°7 per cent.
or, including the extraneous species :—
273 240 33 13°7 per cent.
With regard to geographical distribution, Mr. Jeffreys shows that
352 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
the great majority, viz. 150 species, are still found living in British
seas ; whilst of the 55 species not found living in British seas 32 are
now restricted to more southern, and 23 to more northern seas—
showing, with respect to the Coralline Crag, a gain of 9 northern,
and a loss of 33 southern species.
The total number of species common to the Red Crag and
to/the Coralline Cras isis Seyade ae ae ee ee 186
Or, deducting\extraneous species iis 2) seis eee «46
140
This gives a percentage of species common to the Red and Coralline
Crags of about 62. Or, looking at the percentage of living species
in each, the difference between them is much less, taking even the
smaller percentage due to the exclusion of the extraneous species.
In the Coralline Crag ...... 84 he ae gpe ;
Inthe wRed (Crag 1. ae: 92 | et eee ae ee
ConcLvsion.
In the former part of this paper, I remarked that the Coralline
Crag had, during its latter stages, been subject to a process of slow
elevation, but probably without rising above the sea-level. It had,
however, emerged above the sea at the commencement of the Red-
Crag period, as evinced by the shore-line at the base of the Red Crag
at Sutton (see Pl. VI.), when the Coralline-Crag reef or islet stood
some 40 feet or more above that shore-line. The difference of level
between the lower shore-line and the surface of the London Clay
under the Red Crag in the adjacent district is not more than a few
feet, whence the Red Crag must have been accumulated in a shal-
low sea. Mr. Searles Wood, Jun., considers that the lower division
of the Red Crag is arranged in successive beach-stages. ‘There seems
to me, on the contrary, to be an absence of definite order; and the la-
mination and bedding which he considers referable to beach-action, I
think may in all cases be referred to the variable bedding and oblique
lamination produced by the shifting of shoals and sand-banks at the
bottom of the Red-Crag sea, as was the case with the upper division of
the Coralline Crag (ante, fig. 3, p. 120). Mr. Wood, Sen., has already
expressed his opinion that the peculiar stratification of the Red Crag
must be owing to the constant shifting of the sands and shingle
caused by variable and changing currents ; and this is also the opinion
of Mr. Jeffreys. Shoals may have been formed and removed in
part or wholly by a change of currents, just as now is of constant
occurrence off the present Suffolk coast.
This sea was not only shallow, but was studded with reefs of Coral-
line Crag, amongst which strong and shifting currents set in ; whilst
in winter the more distant Chalk and Tertiary shores were fringed
with ice, which, as it floated off, carried away large, massive flints,
and deposited them in the Red Crag (fig. 21). In the same way ice-
borne blocks and fragments of the Coralline Crag were carried from the
PRHESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 353
Sutton (and possibly the Sudbourne) reef, and scattered over the bed
of the Red-Crag sea (fig. 23). The circumstance of the occurrence
of large masses of flint, covered with Bulan, and of pebbles derived
from distant formations indicate transport, probably by ice-action ;
for the flints are of considerable size and perfectly unrolled. They
seem to have been dropped where they are found; and it is a question
whether the Balani with which many of them are covered may not
have been attached on the coast before their removal. This removal
necessarily requires a certain depth of water, as also would the accumu-
lation and reconstruction by sea-currents of the mass of sand and
comminuted shells forming a great portion of the Red Crag. The
character of the fauna of the Red Crag isin accordance with these
conditions. Jittorima littorea, Purpura lapillus, Cardium edule,
Pholas crispata, Teredo norvegica, and Mytilus edulis clearly indicate
shore-lines ; whilst the several species of Astarte, Trophon, Turri-
tella, Cardita, Nucula, together with the common Pectunculus gly-
cymeris, Pecten opercularis, Mactra ovalis, and others, are confined
to the laminarian and deeper zones.
If we suppose a shoal to have been formed in one part of this
sea-bed, and subsequently, owing to a change in the currents, to
have become subject to a scouring action in another direction, the top
of this shoal would be thrown forward in successive laminee, steep in
proportion to the velocity of the water, and thus form oblique lami-
nation, such as is so common in the Red Crag. Fresh currents may
afterwards have removed other shoals and spread them over these
obliquely laminated beds in a series of horizontal layers, which,
in their turn, may have been scooped and hollowed out, and the
depression filled by a newer accumulation—a case not at all un-
common in the Red-Crag district. This, again, may have been
planed down and re-covered obliquely by a fresh removal of ad-
jacent shoals. In this way we may have an infinite number of
repetitions of the same materials. This constant shifting and re-
adjustment of materials would, at the same time, lead to the heavier
portions, such as the bones, the pebbles, and the phosphatic nodules,
being thrown down and left behind when the lighter materials were
removed, and would thus tend to accumulate them in the basement
beds where we now generally find them.
The consequence of these reconstructions is that a large propor-
tion of the shells are worn or broken, and the mass of them are
finely comminuted. The presence of some entire and double shells
shows that there were more sheltered places. That there were also
intervals of repose and quiet is evident from the circumstance that
thin horizontal seams of very finely laminated clays and sand were
occasionally formed; these we find interstratified at places with the
beds of shelly crag.
I have mentioned that, at Bawdsey, I found a bed of micaceous
sandy clay with laminee covered by ripple-marks, which laminee
were continued in regular succession for a thickness of several feet.
They were formed probably in shallow water (fig. 7). In some cases
beds of clayey sands seem to have been raised above the sea-level,
304. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
or exposed during certain states of the tides till the surface became’
dried and fissured so as to form wedge-shaped cavities filled with the
materials of the beds which were accumulated above them (fig. 8).
In beds deposited under such circumstances, subject to such constant
removal and reconstruction, it is not surprising that it is difficult
to find one in which the shells of the period exist in situ. Possibly
some of the beds at Walton were less frequently disturbed, or may
have been deposited under rather more tranquil circumstances than
elsewhere; still most of those beds are full of comminuted shells,
and many of them show oblique lamination, so that they also were
subject to the action of tides and currents. With a sea of this
character, and with shoals and reefs of the soft friable Coralline
Crag exposed to its action, a large destruction of the latter was in-
evitable ; and the shells of that deposit must consequently have been
transferred in great numbers to the newer beds of the Red Crag
formed around it. To what extent this may have taken place it is
not possible yet to say. I quite agree with Mr. Searles Wood, that
a large number of the shells found in the Red Crag have had this
origin ; but although we can feel little doubt on the subject, yet as
the shells are mostly single valves, and the staining given by the
Red Crag assimilates them to its own fossils, it is difficult to di-
stinguish those which are derived from those which belong to the
deposit. When we meet ‘with the entire or the rolled fragments
of Bryozoa or some of the rare corals, evidently derived from the
Coralline-Crag beds, there can be no doubt of their origin. Still
it is clear that a considerable number of shells lived in the Red-
Crag sea, and that a certain number of new species were introduced.
Many species of bivalves are found double; but this is not always a
proof that they are not extraneous.
I believe also that a large proportion, if not all the coprolites
(so called) of the Red Crag were derived from the Coralline Crag,
as detached ones are found not unfrequently in its mass, and a bed
of them was found to underlie it at Sutton, at the only place where
its base has been exposed (ante, p. 117).
The direction of the currents, judging from the nature of the
foreign materials found in the Red Crag, seems to have been from
the east to south-east. Though the sea was open to the north, the
communication with the south was probably cut off. Innumerable
Balani covered the blocks of Septaria and flint scattered on the
London Clay and Chalk-shores of this Red-Crag sea. Pholades
abounded on its water-line ; and we have seen at Sutton and else-
where that Mytli were common in its shallow waters, while other
genera found shelter in bays and any tranquil places. I can see no
distinction in the organic remains, from the base of the Red Crag to
the top of the lower division. The like abundance of species of
Pectunculus, Mactra, Tellina, Cardium, Fusus, Natica, Purpura, &c.
occurs almost throughout, modified by situation, and having a distribu-
tion sufficiently independent in character to show that it could scarcely
have been dependent upon one source alone, and that a derivative
one, for its fossils, but that there were banks and feeding-grounds
for the various species of Mollusca, which served as centres from
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 305
which they spread, but, in spreading, retamed at the same time
evidences of the grouping they had when living.
After the deposit of the lower division of the Red Crag a subsidence
of some 10 or 12 feet took place, and a new line of cliff, on a higher
level, was formed at Sutton. Even the rise of the tides might almost
be determined ; for we know that the Pholas crispata, the borings
of which are spread over the upper shore and top of the lower cliff,
lives only between water-marks. ‘The perforated space occupies a
zone about 5 or 6 feet deep (see fig. 21).
The increased prevalence of oblique lamination in the upper part
of the lower Red Crag leads to the supposition that the sea was
gradually silting up. To this, however, succeeded a movement of
subsidence causing the erosion, by fresh submarine currents, of the
surface of the lower division, and, as the subsidence gradually con-
tinued, to the accumulation of the upper division of the Red Crag.
From the circumstance of the lower part of these upper sands
being formed of the débris of the previously deposited lower Red
Crag, the mineral character is very similar; but in the ascending
series, formed as the sea-bed gradually became more depressed, the
sands are finer, they lose their red colour, and they pass upwards
into fine micaceous sands and grey clays, in which the Testacea are
constantly found on the spot where they lived.
These sands and laminated clays (the Chillesford series) covered
up and levelled the whole of the various beds beneath them, spread-
ing over them all through Suffolk and Norfolk.
The difference of age which the distinctive characters of the Red
and Coralline Crags might suggest does not hold when each is
viewed separately in relation to the fauna of the present period.
There must have been other causes than mere lapse of time and de-
scent to account for this variation in their respective faunas; and
this probably was owing both to the variation of the level of the bed
of the sea, to which we have directed attention, and by which many
of the deeper-water Mollusca must have been destroyed within our
area, and also to the influx of more northern or north-easterly
currents, and the increased cold, indicated by the physical pheno-
mena, bringing in a more northern fauna. It is a question of tem-
perature rather than of time.
The absence of essential difference of age between the two crags
is also apparent in their correlation with the two upper Crags of
Antwerp, with both of which they show a close relationship—the
lower one of the two being probably of the age of the Coralline,
and the upper one having a near analogy with the Red Crag.
Species com-
Antwerp beds, montothe Proportion of
number of Antwerp beds RedsCrag
species. and the species.
i. Red Crag
Bo | Sables jaunes 197 138 74 per cent.
Scaldisien 1 scbleseris... 187 122 on
Diestien ... Sables noirs.. 228 61 26
Common to the Sables jaunes and gris 139, or 75 per cent. ‘i
We will, however, consider more fully the relations of the Belgian
356 PROCEEDINGS OF THE GEOLOGICAL SOCINTY.
Crags with those of England after treating of the Norwich Crag.
On the latter subject we must make a few observations in reference
to that portion of it which extends into Suffolk. I have shown
that the Red Crag 8. and 8.W. of Sudbourne and Iken is sepa-
rated from that to the northward by a ridge of Coralline Crag, and
that the fossils of the Red Crag take then a more littoral character
and already present at Aldborough a somewhat intermediate type—
the rich fauna of Sutton and Walton having gradually become
poorer, though the shells are still all Red-Crag species, and that
species of Mactra, Mya, Mytilus, and Cardiwm have become more
common. After passing Aldborough the Crag puts on another type;
the littoral shells, especially Littorina littorea, Mya, and Mactra,
largely predominate ; but still, out of 44 species I have found in the
pits between Aldborough and Southwold, there are only two which are
not found in the Red Crag :—the one, Paludina lenta, being a fresh-
water and therefore a local shell *; the other, Astarte borealis, being
a shell of northern type, which here first makes its appearance, and
whose range may have been restricted by the Thorpe ridge of Coral-
line Crag.
The Mammalian remains found at Thorpe and Southwold cannot
be compared with Red-Crag fossils, which are mostly extraneous.
At the same time I would call attention to the occurrence of the
teeth of Mastodon in the Coralline Crag of Sutton, in the Red Crag
of the same district, and in the Crag at Southwold.
Further the stratigraphical relation of the beds is alike in the
two districts. At Chillesford and Iken we find the Chillesford
clays and sands overlying the Red Crag ; and in the same way we
find at Southwold a crag, which is probably the equivalent of the
upper division of the Red Crag, immediately underlying clays which —
contain similar fossils to those in the Chillesford district. It is pos-
sible, also, that in the northern area, as well as in the southern,
there are two subdivisions, of which the beds at Wangford and
Thorpe may be the lower, whilst those at Bulchamp or Southwold
may represent the upper.
In my next communication, I propose tracing the same horizon of
the Chillesford Clay into Norfolk, and to show its relation to the
Crag-beds of that district and their relation to the Crags of Suffolk.
* Mr. A. Bell has since found this shell in the Red Crag at Waldringfield.
DONATIONS
TO THE
LIBRARY OF THE GEOLOGICAL SOCIETY.
From January 2nd to March 31st, 1871.
I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.
Academy (Journal). Vol.ii. No.15. December 1870.
American Journal of Science and Arts. Third Series. Vol. i.
Nos. 1 & 2. January and February 1871.
J.D. Dana.—On the Quaternary, or Post-tertiary, of the New Haven
Region, 1.
G. J. Brush.—On Gahnite from Mine Hill, Franklin Furnace, New
Jersey, 28.
A. C. Twining.—Harthquake of October 20th, in North-eastern
America, 47.
T. S. Hunt.—Notes on Granitic Rocks. Part i., 82.
E. B. Andrews.—Lower Carboniferous Limestone in Ohio, 91.
Baron yon Richthofen.—On the existence of the Nummulitic forma-
tion in China, 110.
American Naturalist. Vol. iv. Nos. 11&12. January and Febru-
ary 1871.
J.S. Newberry.—The Ancient Lakes of Western America: their
Deposits and Drainage, 641.
Atheneum (Journal). Nos. 2252-2264. December 1870 to March
1871.
Berlin. Monatsbericht der kénigl.-preussischen Akademie der Wis-
senschaften zu Berlin. September to December 1870.
G. Rose.—Ueber einen angeblichen Meteoritenfall von Murzuk in
Fezzan, 804.
—. January 1871.
VOL. XXVII.—PART I. 2¢
858 DONATIONS.
Berwickshire Naturalists’ Club. Proceedings. Vol. vi. No. 2.
Presented by Geo. Taiz, Esq., PGS.
British Coal and Iron Trades’ Advertiser and Directory. Vol. i.
Nos. 5 & 6.
Buenos Aires. Anales del Museo Piblico de Buenos Aires. En-
trega Septima (Vol. i. part 1).
H. Burmeister.—Monografia de los Glyptodontes, 1.
Calcutta. Asiatic Society of Bengal. Journal. New Series. Vol.
xxxix. Nos. 164 & 165.
. ——. Proceedings. Nos.9&10. September and Novem-
ber 1870.
D. Waldie.—Analysis of a New Mineral from Burmah, 279.
Canadian Naturalist and Quarterly Journal of Science. New Series.
Vol. vy. No: 2:
T. Macfarlane.—On the Origin and Classification of Original or Crys-
talline Rocks. Part i11., 159.
T. Sterry Hunt.—On the Geology of Hastern New England, 198.
Chemical News. Vol. xxii. Nos. 577-579. Vol. xxiii. Nos. 580—
590. December 1870 to March 1871.
Chemical Society. Journal. Second Series. Vol. ix. January
and February 1871.
Colliery Guardian. Vol. xx. Nos. 521 & 522 (December 1870) ; and
Vol. xxi. Nos. 523-533 (January to March 1871).
Darmstadt. Notizblatt des YVereins fir Erdkunde. Folge 3.
Heft ix.
Dorpat. Archiv fiir die Naturkunde Liv-, Ehst-, und Kurlands.
Erste Serie, Band vi. erste Lieferung. Zweite Serie, Band vii.
zweite Lieferung. 1870.
Sitzungsberichte der Dorpater Naturforscher-Gesellschaft.
Dritter Band, erstes Heft. 1869.
Edinburgh. Royal Society. Proceedings. Vol. vii. No. 80.
A. Geikie-—On the Geological Structure of some Alpine Lake-
Basing, 33.
T. Brown. On the Old River Terraces of the Earn and Teith,
viewed in connection with certain Geological Arguments for ine
Antiquity of Man, 41.
Turner.—On the Bones of a Seal found in Red Clay near Grange-
mouth, with Remarks on the Species, 105.
————, , Transactions. Vol. xxvi. Part 1.
T. Brown.—On the Old River Terraces of the Earn and Teith,
viewed in connection with certain Proofs of the Antiquity of Man,
149 (1 plate).
DONATIONS. 359
Florence. Bollettino del Reale Comitato Geologico d’Italia. Nos.
9-12. September to December 1870.
I. Coechi.—Del Granito di Val di Magra, 229.
Di un lembo di terreno Titonico in Val di Magra, 235.
G. Curionii—Osservazioni geologiche sulla Val Trompia, 249.
G. A. Pirona.—Sui terreni di sedimento dei Colli Euganei, 257.
I. Cocchi—Note geologiche sopra Cosa, Orbetello e Monte Argen-
tario nella Provincia di Grosseto, 277.
Geological Magazine. Vol. viii. Nos. 1-3. January to March
1871.
A. H. Green.—The Geological Bearings of Recent Deep-sea Sound-
ings, l.
R. Tate.—A Census of the Marine Invertebrate Fauna of the Lias, 4.
J. C. Ward.—The Development of Land, 11.
J. Croll—The Transport of Wastdale Crag Blocks, 15.
J. Hopkinson.—On Dicellograpsus, a new Genus of Graptolites, 20
(1 plate).
ls a) ae the Diamond Fields of South Africa, 49.
G. S. Brady.— Notes on Fossil Post-Tertiary Ostracoda, 60 (1
late).
oF ese of Denudation, seen in the Coprolite Pits of
Cambridgeshire, 65.
H. Woodward.—Notes on a New British Cystidean, 71.
J. Croll.—On a method of determining the mean Thickness of the
Sedimentary Rocks of the Globe, 97.
H. Woodward.—On Euphoberia Brownit, a new Myriapod from the
Coal-measures of Scotland, 102 (1 plate).
. On some new Phyllopodous Crustaceans from the Paleozoic
Rocks, 104 (1 plate).
C. E. de Rance.—On the two Glaciations of the Lake District, 107.
J. Aitken.—On Faults in Drift at Stockport, Cheshire, 117.
S. G. Perceval—On the Occurrence of Websterite at Brighton,
121,
Prof. Shaler. On the Parallel Ridges of Glacial Drift in Hastern
Massachusetts,’ noticed, 27.
©. Moore-— On the Mammalia from Drift Deposits near Bath,’
noticed, 28.
Geological-Survey Memoir, noticed, 73.
A. Bryson.— On Pholas-borings,’ noticed, 73,
Prof. Kjerulf—‘ On the Terraces of Norway,’ noticed, 75.
G. Lindstrém.— On some Operculated Corals, Silurian and Recent,’
noticed, 122.
‘The Geological Survey of India,’ noticed, 126.
‘The Rocky Mountains, Geological Explorations,’ noticed, 127.
M‘Andrew’s ‘ Dredgings in the Gulf of Suez,’ noticed, 128.
W. C. Lucy.—‘ On the Gravels of the Severn, Avon, and Evenlode,’
reviewed, 29.
F. V. Hayden.— Geological Reports’ (American), reviewed, 32.
Savile’s ‘Truth of the Bible,’ &c., reviewed, 76.
“Devonshire Association for the Advancement of Science,’ reviewed,
78.
‘Royal Geological Commission of Italy,’ reviewed, 80.
R. B. Smyth.— Report on the Geological Survey of Victoria,’ re-
viewed, 129.
Neues Jahrbuch fiir Mineralogie, &c., reviewed, 131.
2¢c2
360 DONATIONS.
Geological Magazine. Vol. viii. Nos. 1-3 (continued).
Ball’s ‘Guide to the Western Alps,’ reviewed, 182,
Reports and Proceedings of Socicties, 35, 82, 134.
Correspondence, 39, 88, 142.
Obituary, 45.
Miscellaneous, 48, 144.
Geologists’ Association. Annual Report for 1870. (2 copies.)
Iron and Coal Trades Review. Vol. iv. Nos. 147 & 148 (De-
cember 1870); and Vol. v. Nos. 149-159 (January to March
1871).
Iron and Steel Institute. Journal. Vol. i. No. 1. February 1871.
Mineral Statistics of Great Britain and Ireland, 6._
W. Adams.—On the Geological Features of the South-Wales Coal-
field, 13.
G. J. Snelus—The Conditions of Carbon and Silicon in Iron and
Steel, 28.
F. Kohn.—Production of Alloys of Iron and Manganese, 70.
Linnean Society of London. Journal. Zoology. Vol. xi. No. 50.
1871.
——. Proceedings. Session 1870-71. November to December.
Liverpool. Abstract of the Proceedings of the Liverpool Geological
Society. Session the Eleventh. 1869-70. (2 copies.)
G. H. Morton.—Anniversary Address, 3.
C. Ricketts.—Geological Observations in the Neighbourhood of
Exeter, 33.
A. N. Tate.—The Chemistry of Granite, as Hlustrating the Origin of
Granitic Rocks, 37.
A. Morgan.—The Formation of Metalliferous Veins, 37.
R. Bostock.—The Mersey and the Dee, their former Channels and
and Change of Level, 41.
S. Cooke.—On Deep-Sea Dredgings in the Atlantic, 49.
C. Ricketts.—The Section of Strata exposed on the Huyton and St.
Helen’s Branch Railway, 56.
Liverpool. Transactions of the Historic Society of Lancashire and
Cheshire. New Series. Vol. x. Session 1869-70.
London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xli. Nos. 270-272. January to March 1871. From
Dr. W. Francis, F.G.S.
J. Ball.—On the Cause of the Motion of Glaciers, 81.
J. A. Phillips.—On the Chemical Composition and Microscopic Con-
stitution of certain Cornish Rocks, 87.
E. Hull.—On the Geological Age of Ballycastle Coal-field, and its
relation to the Uarooniferous Rocks of the West of Scotland,
155.
DONATIONS. 361
London Institution. Journal. Vol.i. Nos.1-3. January to March
1871.
J. Morris.—On Precious Metals and Precious Stones, 21.
Longman’s Notes on Books. Vol. iv. No. 64.
Monthly Microscopical Journal. Vol. v. Nos. 25-27. January to
March 1871.
Munich. Sitzungsberichte der konigl.-bayer. Akademie der Wissen-
schaften zu Miinchen. 1870. Band iu. Hefte 1 & 2.
Nature (Journal). Vol.ii. Nos.60-72. January to March 1871.
W. Boyd Dawkins. Paleontology of Man, 143.
T. M. Read.—EHozo6n canadense, 146.
W. B. Carpenter.—Eozoén canadense, 185.
W. M. Williams.—Papers on Iron and Steel, 211.
On the Geology of Nova Scotia, 214.
W. Thomson.—The Continuity of Chalk, 225.
Principal Dawson.—Kozoon canadense, 267, 287.
Earthquakes at Fiume during the year 1870, 269.
G. H. Kinahan.—The Cretaceous Period, 286.
D. Forbes.—The Nature of the Earth’s Interior, 296.
T. M‘K. Hughes.—The Cretaceous Period, 308.
A. R. Wallace.—Theory of Glacial Motion, 309.
T. M‘K. Hughes.—Caves near St. Asaph, 327.
Paleontographical Society. Vol. xxiv. Issued for 1870. 1871.
(2 copies.)
HK. W. Binney.—The Flora of the Carboniferous Strata. Part ii.
(6 plates.)
T. Wright.—The Cretaceous Echinodermata. Vol. i. Part iv. (10
plates. )
T. Davidson.—The Fossil Brachiopoda. Part 7. No. 4 (Silurian).
(15 plates.)
S. V. Wood.—The Eocene Mollusca. Partiv. No. 3 (Bivalves). (5
plates.)
R. Owen.—The Fossil Mammalia of the Mesozoic Formation. (4
plates.)
Paris. Comptes Rendus hebdomadaires des Séances de Académie
des Sciences. Deuxiéme Semestre 1870. Tome lxxi. Nos. 9-26.
S. Meunier—Sur les rapports de l’Astronomie physique avec la
Géologie, 541.
Relations stratigraphiques entre diverses roches météoriques
743, 771. .
Fouqué.—Etudes des gaz voleaniques de Santorin, 902.
S. Meunier.—Sur le mode de solidification du globe terrestre, 956.
——, ——. Premier Semestre 1871. Tome lxxii. Nos. 1-9.
S. Meunier.—Structure du globe d’ot proviennent les météorites,
ie
——. Mode de rupture de l’astre d’ot dérivent les météorites, 125,
——. Situation astronomique du globe d’ou dérivent les météorites,
183.
362 DONATIONS.
Paris. Comptes Rendus hebdomadaires des Séances de l’Académie
des Sciences. Premier Semestre 1871. Tome Ixxii. Nos. 1-9
(continued). :
Elie de Beaumont.—Observations sur un tubercule de fer natif,
d’origine évidemment météorique, trouvé dans le calcaire juras-
sique, 187.
Revue des Cours Scientifiques de la France et de ’Etranger.
Septicme Année. Nos. 42-50. September 1870 to March 1871.
Photographic Journal. Nos. 221-223. January to March 1871.
Quarterly Journal of Science. No. 29. January 1871.
Quekett Microscopical Club. Journal. No. 13. January 1871.
Royal Asiatic Society of Great Britain and Ireland. New Series.
Vol. v. Part 1.
Royal Society. Proceedings. Vol. xix. Nos. 124-126.
R. Owen.—On the Fossil Mammals of Australia. Part iv. Dentition
and Mandible of Thylacoleo carnifex, with Remarks on the argu-
ment for its Herbivority, 95.
E. Hull.—On the Extension of the Coal-fields beneath the Newer
Formations of England; and the succession of Physical Changes
whereby the Coal-measures have been reduced to their present
dimensions, 222.
J. H. Pratt.—On the Constitution of the Solid Crust of the Harth,
223.
N.S. Maskelyne.—On the Mineral Constituents of Meteorites, 266.
W. C. Williamson.—On the Organization of the Calamites of the
Coal-measures, 268.
Society of Arts. Journal. 117th Session. Vol. xix. Nos. 944-956.
Student and Intellectual Observer. New Series. Vol. i. No. 5.
January 1871.
M. E. Collomb.—Glacial Marks near Fontainebleau, 527.
Turin. Atti della Reale Accademia delle Scienze di Torino. Appen-
dice al volume iv.
—. —. Vol.v.
L. Lanino.—Sulla costituzione geologica dei terreni adiacenti alla
strata ferrata Foggia-Napoli nel tronco Bovino-Ponte, 69.
GastaldiimRaccolta di stromenti di pietra delle adiacenze del Baltico ;
dono di 8S. M. il Ré, 841.
. Alcune antiche armi e strumenti di pietra e di bronzo o rame
provenienti dall’ Egitto, 862.
. Bollettino Meteorologico ed Astronomico del Regio Osserva-
torio dell’ Universita di Torino. 1869.
Notizia Storica dei Lavori fatti della Classe di Scienze
Fisiche e Matematiche della Reale Accademia delle Scienze di
Torino negli anni 1864 e 1865.
DONATIONS. 363
Vienna. Anzeiger der k.-k. Akademie der Wissenschaften in Wien.
1870, Nos. 28 & 29. 1871, Nos. 1-6.
Jahrbuch der k.-k. geologischen Reichsanstalt. Band xx.
Nos. 2&3. 1870.
M. Neumayr.—Ueber einige neue oder weniger bekannte Cephalo-
poden der Macrocephalen-Schichten, 147 (8 plates).
F, Karrer.—Ueber ein neues Vorkommen von oberer Kreideformation
in Leitzersdorf bei Stockerau und deren Foraminiferen-Fauna, 157
(2 plates).
D. Stur.—Beitrige zur Kenntniss der Dyas- und Steinkohlen-For-
mation im Banate, 185.
F. y. Andrian.—Geologische Studien aus dem Orient, 201.
ix. M. Paul.—Das Gebirge von Homonna, 217.
Das Karpathen-Sandsteingebiet des nodrdlichen Ungher und
Zempliner Comitates, 243.
Beitrage zur Kenntniss der Congerien-Schichten Westslavo-
niens und deren Lienitfuhrung, 251 (1 plate).
E, Tietze.—Beitriige zur Kenntniss der alteren Schichtgebilde Karn-
thens, 259.
A. Pichler.—Beitrice zur Geognosie Tirols, 273.
Ti. Abich.— Die Reihen-Vulcan-Gruppe des Abul und des Samsar auf
dem kaukasischen Isthmus, 275.
G. Tschermak.—Ueber den Trinkerit, ein neues fossiles Harz yon
Carpano in Istrien, 279.
O. Boettger—Revision der tertiiren Land- und Siisswasser-Ver-
steinerungen des nordlichen Bohmens, 283 (1 plate).
D. Stur.—Beitrage zur Kenntniss der stratigraphischen Verhaltnisse
der marinen Stufe des Wiener Beckens, 303.
T. Fuchs.—Beitrige zur Kenntniss fossiler Binnenfaunen. III. Die
Fauna der Congerien-Schichten von Radmanest, 304 (4 plates).
_F. v. Hochstetter—Die geologischen Verhiltnisse des 6stlichen
Theiles der europaischen Turkei, 305 (1 plate).
Vienna. Verhandlungen der k.-k. geologischen Reichsanstalt. 1870,
Nos. 15-18.
J. Haast.—Ein Ausbruch des Vulcanes Tongariro auf Neu-Seeland,
304.
E. Tietze.—Ueber ein Vorkommen von gediegenem Kupfer zu
Maidanpeck in Serbien, 304.
G. C. Laube.—Die Echinoiden der osterreichisch-ungarischen oberen
Tertirablagerungen, 313.
F. Foetterle-—Die Verbreitung der sarmatischen Stufe (Cerithien-
Schichten) in der Bukowina und der nérdlichen Moldau, 314.
T. Fuchs.—Die Fauna der Congerien-Schichten von Tihany und
Kup, 320.
C. v. Hauer.-—Seifenstein von Fohnsdorf in Steiermark, 320.
H. Tietze.— Ueber das Vorkommen eines sogenannten Glammganges
zu Maidanpeck in Serbien, 321.
Auftindung yon braunem Jura bei Boletin in Serbien, 323,
——. Auffindung von Neocom und Turon im nordéstlichen Serbien,
324.
M. Neumayr.—Ueber die Hornsteinkalke des siidlichen karpathischen
Klippenzuges, 324.
J. Noth.—Nachrichten tiber die Resultate von Bohrungen auf Erdol
bei Kleezany und Ropianka in Westgalizien, 335,
364 DONATIONS.
Vienna. Verhandlungen der k.-k. geologischen Reichsanstalt. 1870,
Nos. 15-18 (continued).
F. v. Vivenot.—Milkroskopische Untersuchung des Syenites von
Blansko in Mihren, 336.
C. v. Hauer.-—Gesteine von Macska Rév, 337.
K. Tietze.—(1) Auftindung von Orbitulitengestein bei Bersaska im
Banat, 338. :
(2) Cornubianite des Szaszka-Thales in Serbien, 338.
(3) Ueber den Milanit, ein neues Mineral, 339.
F., Posepny.—Alleemeines tiber das Salzvorkommen Siebenbirgens,
339.
1871, Nos. 1-3.
E. von Mojsisovics—Ueber die muthmassliche Verbreitung der
kohlenftihrenden Haringer Schichten im Unter-Innthale, 3.
A. Koch.—Beitrag zur Kenntniss der geognostischen Verhaltnisse
des Vrdniker Gebirges in Ostslavonien, 15.
A. de Zigno.—Halitherium, dann Mastodon arvernensis in den Ter-
tiargebilden im Venetianischen, 15.
A. Kornhuber.—Ueber einen neuen fossilen Saurier aus Lesina, 16.
C, v. Hauer.—Die Braunkohlen des Falkenauer Beckens in Boh-
men, 20.
M. Neumayr.—Die Fauna der Schichten mit Aspidoceras acanthicum,
Oppel, im Nagy-Hagymas-Gebirge in Siebenbiirgen, 21.
K. von Mojsisovics.—Ueber die Triasbildungen der Karavankenkette
in Karnthen, 25.
M. Gross.—Ueber das Breber Mineralwasser, 33.
K. Peters.—Unterkiefer eines Dinotheriwm giganteum (D. medium),
Kaup, 34.
S. Douglass.—Petrefactenfuhrender Kalkstein aus dem Gargellenthal
in Vorarlberg, 35.
J. Woldtich.—Quarzit, Graphit und Aphanit in der Gneissformation
bei Gross-Zdékau im Bohmerwalde, 35.
F. Posepny’.—Ueber das Hisenstein- Vorkommen yon Gyalar in Sie-
benburgen, 39.
—. Ueber die Erzlagerstitte von Kisbanya in Siebenbirgen, 40.
G. Stache.—Ueber die Versorgung der Stadt Bozen mit Trinkwasser,
4].
II. PERIODICALS PURCHASED FOR THE LIBRARY.
Annals and Magazine of Natural History. Fourth Series. Vol. vii.
Nos. 37-39. January to March 1871.
H. G. Seeley.—Additional Evidence of the Structure of the Head
a a from the Cambridge Upper Greensand, 20 (2
plates).
H. Burmeister.—On Saurocetes argentinus, a new Type of Zeuglodon-
tide, 51 (1 plate).
H. Woodward.—The Tertiary Shells of the Amazons Valley, 59,
101 (1 plate).
EK. Ray Lankester.—On Recent and Fossil Corals, 66.
DONATIONS. 365
Annals and Magazine of Natural History. Fourth Series. Vol. vii.
Nos. 37-39. January to March 1871 (continued).
pce Cope.—On the Structure of the Crania of Reptilia and Batra-
chia, 67.
A. Hancock and T. Atthey.—Description of a considerable portion of
a mandibular ramus of Anthracosaurus Russelli; with Notes on
Loxomma and Archichthys, 73 (1 plate).
H. J. Carter.—On Fossil Sponge-spicules of the Greensand compared
with those of existing Species, 112 (4 plates).
E. Billings.—Notes on the Structure of the Crinoidea, Cystidea, and
Blastoidea, 142.
E. Parfitt.—On a Species of Arenaceous Foraminifer (?) from the
Carboniferous Limestone of Devonshire, 158 (1 plate).
H. B. Brady.—On Saccammina Carteri, a new Foraminifer from the
Carboniferous Limestone of Northumberland, 177 (1 plate).
A. Hancock and T. Atthey.—A few Remarks on Dypterws and
Ctenodus, and on their Relationship to Ceratodus Forstert, Krefit,
190 (2 plates).
A. Ginther.— Ceratodus and its Place in the System, 222.
Paleontographica: herausgegeben von Dr. W. Dunker und Dr. K.
A. Zittel. Band xix. Lief. 4 & 5,
O. Speyer.—Die Conchylien der Casseler Tertidrbildungen, 159 (4
plates).
Schenk.—Beitrage zur Flora der Vorwelt, die fossile Flora der nord-
westdeutschen Wealdenformation, 203 (8 plates).
IIT. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.
Abich, H. “tudes sur les Glaciers Actuels et Anciens du Caucase.
Premiére Partie. S8vo. Tiflis, 1870.
Ansted, D. T’. Considerations on the Selection of Building Sites.
4to. 1871.
Ansted, D. T. Considerations on the Selection of Building Sites.
Ato. 1871. Presented by the Royal Institution of British Archi-
tects.
Barry, R. Address on the Opening of the School of Mines at Bal-
larat (Victoria). Svo. Melbourne, 1870.
Blyth, E. On Mr. W. Theobald and Dr. Falconer.
Brigham, W. T. Historical Notes on the Earthquakes of New
England, from 1638 to 1869. 4to. 1871.
Broome, G. Report on the Canadian Phosphates considered with
reference to their application to Agriculture. Part I. 8vo.
Montreal, 1870.
366 DONATIONS.
Carter, H. J. On Fossil Sponge-Spicules of the Greensand compared
with those of existing species. Syo. 1871. Presented by Prof.
P. Martin Duncan, F.R.S. Se.
Cov, EH. T. Geological Survey of Indiana, made during the year
1869 (with Maps). 8yvo. Indianopolis, 1869.
Croll, J. On the Mean Thickness of the Sedimentary Rocks of the
Globe. 8vo. 1871.
oat On the Transport of the Wastdale Crag Blocks. 8vo. 1871.
Y Cuvier, Baron G. A Discourse on the Revolutions of the Surface of
the Globe. 8vo. 1829. From W. Whitaker, Esq., F.GS.
Dall, W. H. <A Revision of the Terebratulide and Lingulids, with
Remarks on, and Description of, some Recent Forms. 8vo.
1870.
De Rance, C. E. Geology of the Country between Liverpool and
Southport, and Explanation of Geological Survey Map, Sheet 90,
S.E. Presented by the Geological Survey of England and Wales.
Dewalque, G. Coup d’ceil sur la Marche des Sciences Minérales en
Belgique. 8vo. 1870.
Dublin University Magazine, for November 1870, containing a paper
by H. Pearce “On a Group of Old Stones.” From H. Peuree,
Eisq., F.GS.
Forbes, Prof. Edward, a Lithographic Portrait of. Presented by Prof.
Tennant, F.GS.
Fuchs, T. Ueber Dreessenomya, ein neues Bivalvengenus aus der
Familie der Mytilaceen. 8vo. 1870.
Geinitz, H. B. Ueber fossile Pflanzen aus der Steinkohlenformation
am Altai. 8vo. Leipzig, 1871.
Gumbel, C. Vergleichung der Foraminiferenfauna aus den Gosau-
mergeln und den Belemnitellen-Schichten der bayrischen Alpen.
8vo. 1870.
Guy, W. A. On the Claims of Science to Public Recognition and
Support; with Special Reference to the so-called “Social
Sciences.” 8vo. 1870.
Hall, T. M. On Certain Variations of Temperature during the
Solar Eclipse of December 22nd, 1870. 8yo. 1870.
Hauer, F. von. Geologische Uebersichtskarte der dsterreichisch-
ungarischen Monarchie. Blatt No.1 & 2, and explanation. From
the Geological Survey of Austria.
Hector, James. Sketch-map of the Geology of New Zealand.
DONATIONS. 367
Hector, James. The Fourth and Fifth Annual Report on the Colonial
Museum and Laboratory; together with a Report on the Results
of Certain Analyses. 8vo. New Zealand, 1869-70.
Holmes, F. 8. Phosphate Rocks of South Carolina and the “ Great
Carolina Marl-Bed.” 8vo. 1870. Presented by Triibner and Co.
Hopkinson, J. On Dicellograpsus, a new Genus of Graptolites. 8vo.
1871.
Institution of Civil Engineers. Supplement to the Second Edition
of the Library Catalogue. 8vo. 1870. From that Institution.
Jones, T. Rupert. On the Diamond Fields of South Africa. 8vo.
1871.
Jordan, H. K. A Catalogue of British Mollusca. S8vo. Bristol,
1866-70. From J. Gwyn Jeffreys, Esq., PRS. Se.
Lartet, E., et H. Christy. Cavernes du Périgord. Objets Gravés et
Sculptés des Temps Pré-Historiques dans Europe Occidentale.
8vo. Paris, 1864. From H. B. Woodward, Esq., F.GS.
Lea, I, A Synopsis of the Family Unionide. 4to. Philadelphia,
1870.
_ Levi, L. An Introductory Lecture to the Department of the Even-
ing Classes at King’s College. S8vo. 1870. From Professor P.
Martin Duncan, FBS.
Lyell, C. The Student’s Elements of Geology. 8vo. 1871.
Mineral Statistics of the United Kingdom of Great Britain and
Ireland for the Year 1869, with an Appendix by R. Hunt. 8vo.
1870. Presented by the Geological Survey of Great Britain.
Mylne, R. W. A Geological Map of London and its Environs.
1871.
Ordnance Survey Maps of the United Kingdom, 1-inch scale. Scot-
land: Sheets 13, 17, 48, 67. Ireland: Sheets 23, 26, 77, 78,
85, 88.
, 6-inch scale. Aberdeenshire: Sheets 90, 91,99, 100. De-
von: 117, 128. - Isle of Man: 1-19. Kent: 3-14, 18-22, 31,
32, 42,43. From the Secretary of State for War.
Piggot, J. Note on the History and Distribution of Gold, Silver,
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Reports on the Geological Survey of British Guiana, taken from the
‘Colonist’ Newspaper. 8vo. Demerara, 1870. Presented by
J. G. Sawkins, Esq., F.GS.
Report. Thirty-fourth Annual Report of the Council of the Art-
Union of London, with List of Members. S8vo. 1870. From the
Art-Union of London.
368 DONATIONS.
Royal College of Physicians. A List of the Fellows, Members,
Extra-Licentiates, and Licentiates. S8vo. London. 1871.
Switzerland, Geological Survey Map of. Sheets Nos. 6, 7 & 22, with
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Matériaux pour la Carte Géologique de la Suisse. Septieme
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A. Jaccard.—Supplément 4 la Description Géologique du Jura Vau-
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Huitiéme Livraison. From the Swiss Geological
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J. B. Greppin.—Description Géologique du Jura Bernois et de
quelques districts adjacents.
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Victoria. Reports of the Mining Surveyors and Registrars, Quarter
ending 30th September 1870. From the Colonial Government,
Victoria.
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the Colony. Second Session. 4to. Melbourne, 1870. rom the
Colonial Government, Victoria. '
Walker, J. F. On Secondary Species of Brachiopoda. 8vo. 1870.
Wynne, A. B. On the Geology of Mount Tilla in the Punjab. 8vo.
1870.
Zirkel, F. Geologische Skizzen yon der Westkiiste Schottlands.
8vo. 1871.
Zittel, K. A. Ueber den Brachial-Apparat bei einigen jurassischen
Terebratuliden und iiber eine neue Brachiopodengattung Dime-
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IV. BOOKS &c. PURCHASED FOR THE LIBRARY.
Quenstedt, F. A. Petrefactenkunde JDeutschlands. I. Abth.
Band ii. Heft 4, with Atlas. 1871.
Stoppani, A. Paléontologie Lombarde, publiée avec le concours de
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L bis Z. 8vo. Breslau, 1870.
THE
QUARTERLY JOURNAL
OF
THE GEOLOGICAL SOCIETY OF LONDON.
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
Aprin 26, 1871.
Robert Russell, Esq., of the Geological Survey of England and
Wales, was elected a Fellow of the Society.
The following communications were read :—
1. On a New Spectres of Conan from the Rep Cra of WALDRINGFIELD.
By P. Martin Duncan, M.B., F.R.S., F.G.S., Prof. Geol. King’s
Coll. Lond., &c.
Tue solitary specimen of a compound Madreporarian which forms
_the subject of this communication, was found by Mr. Alfred Bell at
Waldringfield, and was sent to me for description. The coral is
interesting, because it belongs to a reef-forming type which has
lasted from the Eocene to the present day, and which, doubtless,
some day or other, will prove to be much more ancient.
The specimen had been considerably rolled and worn before its
deposition amongst the other materials constituting the Red Crag,
and it must therefore be regarded as a remanié fossil. It becomes,
therefore, rather important that the geological age of the form should
be determined ; but as its mineralization affords no assistance in
this inquiry, any satisfactory results must depend upon the correct
appreciation of its paleontology.
Genus SotenastRaA, Milne-Edwards & Jules Haime, 1848.
Solenastreea Prestwichi, sp. nov.
The corallum is short, and the corallites are crowded.
The upper surface is very irregular, and the corallites differ in
size.
VOL. XXVII.—PART I. 2D
» 370 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 26,
The corallites enlarge rapidly after having originated as buds.
The epitheca is very stout, and is strongly marked by transverse
ridges and intermediate depressions.
The costee are visible on the upper surface of the corallum.
The calices are unequal, usually circular in outline, shallow, with
stout margins. They project but slightly.
The columella is well developed and large.
The septa are in six systems, and there are three cycles of them
in each. The primary and secondary septa are nearly equal, and
reach the columella. The septa of the third cycle are small, and do
not reach far inwards. The endothecal dissepiments are oblique
and scanty.
Diameter of calices 4, to 3, inch.
The Solenastrece no longer inhabit the European seas, and no
trace of them occurs in the dredgings of the North Atlantic Sea,
of the Lusitanian coasts, and of the Mediterranean. They are not
deep-sea forms, but are compound epithecate and exothecate corals
suited for reef-building.
They abound in the reefs of the Red Sea, of the Indian and Great
Ocean, and amongst the West-Indian reefs.
The fossil species have been found in the following localities :—
Eocene—Fort Saint Pierre, Ghent*.
Oligocene—Monte Grumi, Montecchio Maggiore, Monte Viale, and
Monte delle Carrioli, in the District of Castel Gomberto, in Be
Vicentin }.
Brockenhurst and Roydon, in Hampshire t.
Miocene—The Faluns, and Miocene of Turin and of Styria§.
Miocene of Antigua||.
Raised Reefs—Red Sea 4.
The new species differs from the Eocene type by having a well-
marked columella, and in its septal arrangement.
Its small number of septa distinguishes it from the Oligocene
forms.
The well-developed columella and the septal number associate
the new species with the Miocene Solenastrea turonensis, Kd. & H..,
of the Faluns, Turin, Styria, and Antigua, and with the recent s.
Bournon, Ed. & H., Antilles, S. Forskelana, Ed. & H., Red Sea,
S. sarcinula, Ed. & H., eaten Ocean, and S. Ranbern Ed. &
H., Singapore. The closest alliance is with the West-Indian recent
* Solenastrea Verhelsti, Hd. & H., is found amongst the Upper Miocene of
the West Indies.
+ Solenastrea conferta, Reuss, and S. colwmnaris, Reuss, Pal. Stud. iiber die
alteren Tertiar. der Alpen. Wien. Akad. der Wissensch. 1867.
+ Pal. Soc. Lond. P. M. Duncan, 1866.
g Solenastrea turonensis, Hd. & H. Hist. Nat. des Corall. vol. ii. p. 488.
|| ‘ Koss. Corals of West Indies,” Quart. Journ. Geol. Soc. Dec. 1867, and
previous papers.
4 Solenastrea gibbosa, Hd. & H. op. cit. p. 496.
1871.] DUNCAN—NEW CORAL. 371
form S. Bowrnont, Ed. & H.; and S. turonensis, Ed. & H., of the
Faluns is the nearest fossil associate of the new form.
The great change in the physical geography of the European seas
at the close of the Miocene epoch, when they no longer possessed
coral-reef areas, will account for the extinction of the species de-
scribed in this communication ; and the previous extension of those
areas facilitates our comprehension of the distribution of the Solen-
astree in Miocene times, and in the existing reef-faunas,
This new crag-coral was not a member of the London-clay coral-
fauna; for no reef-building forms exist in the remains of that as-
semblage. It belonged to the rich reef-building fauna which suc- -
ceeded that which was associated with Nummulites, and which
lasted in Europe until the progressive upheaval of the Alps and
Western Europe, together with the subsidence of the great northern
barrier, determined the destruction of the assemblage of species by
altering the requisite external physical conditions*,
Discussron.
Mr. Eruermer remarked that the origin of this interesting fossil
seemed uncertain. It appeared, however, to be derived from some
other source, and not to have originally belonged to the Red Crag.
In England the genus was hitherto unknown in beds newer than
those of Brockenhurst. The presence of this single specimen showed
how much we had still to learn with regard to the Crag formation.
It was to be hoped that the coral might eventually be found attached
to some organism from which its age might be determined.
Prof. T. Rupert Jones remarked that he should be glad to hear
of more corals being discovered in the so-called Coralline Crag. He
inquired whether coenepchymatous corals were necessarily reef-
corals, observing that this coral was referred to the Miocene on
account of its presumed reef-forming character. He added that
some of the Foraminifera of the White Crag had the aspect of ex-
isting western Mediterranean forms, and thus supported some of
Prof. Duncan’s remarks.
Mr. Gwyn Jerrreys observed that the distinction between the
fauna of the Coralline and Red Crag was every day diminishing.
The appearance of the fossil seemed to betoken its derivative cha-
racter. Like other speakers, he complimented Mr. Alfred Bell on
his great intelligence in the collection and study of Crag fossils.
Prof. Duncan, in reply, maintained that the differences between
deep-sea and reef-building corals were well established. Around
modern reefs in the deeper sea the forms were quite distinct, and
the deep-sea corals never presented the ccenenchyma distinctive of
the reef-building forms. This, he suggested, might be connected
with the difference in the amount of sea-water with which they
were brought into contact, which in the surf was much greater than
in the almost motionless depths of the sea.
* The species will be figured in my monograph of the Brit. Foss. Corals, Pal,
Soe., which is about to be completed. ¥
2D
372 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
2. Norss on the Minerats of Srrontian, ARGYLLSHIRE.
By Rozert H. Scorr, Esq., F.R.S., F.G.S8.
Wuev I first proposed to visit Strontian, in the year 1866, I consulted
two well-known Scotch geologists as to my chance of picking up
minerals there. The two authorities directly contradicted each other.
One, who was a professed mineralogist, stated that he had spent three
weeks there, and that nothing whatever new was to be found there.
The other was more encouraging, and informed me that whatever I
found was nearly sure to be new.
Greg and Lettsom enumerate a fair series of specimens from thie
‘locality ; but the experience I have gained as to their accuracy as
regards Irish localities, leads me to be somewhat dubious of receiving
all their statements as absolutely correct for out-of-the-way districts,
such as Strontian.
The longest list which has been printed is that given by Mr. Hall
in his Mineralogical Directory, and it is as follows :—
Apophyllite. Calcite. Pyromorphite.
Asbestos. Galena. Sphene.
Baryte. Garnet. Strontianite.
Blende. Harmotome. Tale.
Brewsterite. Pyrites. Zircon.
This list contains no notice of the various feldspars, of which there
are certainly two, Orthoclase and a clear anorthic feldspar, in the
granite, or of the Hornblende and other pyroxenic minerals which
occur in the syenites and crystalline greenstones of the district, and
of which fine, though not perfectly crystallized, specimens, are easily
to be had. Nor does it mention Natrolite in geodes in the trap-
dykes, or Schorl, or either of the micas, white and black, although
very large plates of the former are found on Ben Resipol associated,
as usual, with the garnets for which that mountain is famous.
These latter minerals I have myself seen im situ. Furthermore
there appear to be some doubtful species in the list ; of these [would
only enumerate three, Apophyllite, Tale, and Zircon. No analysis
is given of any of the three from this locality in any of the recog-
nized text-books of Mineralogy. Apophyllite I have never de-
tected among the gangue of the lead-mines. This of course does
not prove much. Tale certainly does not occur anywhere near
Strontian itself; and although from the analogy between the geology
of the district and that of Donegal, in Ireland, I might fairly expect
to find it, I could never trace any beds which bore the slightest re-
semblance to those in which so much Tale and Steatite have been
discovered in the north-west of Ireland. I myself believe that the
name of Tale has been loosely given to the large plates of white mica
to which I have alluded, an error in nomenclature so very common
in collections of Cornish minerals.
As to Zircon I have searched for it most carefully, and can only
say that, as Greg and Lettsom admit the crystals from Criffel said to
be Zircon to be really Sphene, I believe a similar qualification might
with advantage be given to the alleged occurrence of Zircon at
Strontian, and that it is as yet not proven.
1871.] SCOTT—ARGYLLSHIRE MINERALS. 373
The foregoing statements however, are, of much less interest than
the information which can be gained about the minerals for which
the locality has been so long known. These are Strontianite, Har-
motome, Brewsterite, and Calcite. They are all found in a lode
which runs along the edge of the granite, in many places one wall
being granite and the other gneiss. The latter rock presents in the
neighbourhoodof the lode a remarkable porphyritic appearance, caused
by the abundance of large crystals of Orthoclase which it contains *.
The mines were first worked more than 150 years ago, by the Duke
of Norfolk and Co. Then the York Building Company in 1722 took
a lease of them from Sir Alexander Murray, of Stanhope, the pro-
prietor. This gentleman had done a great deal to develop the re-
sources ef that district of Argyllshire. He obtained the services of
a Mr. Bruce to survey the property; and an elaborate map of the
district was published by him in 1733. Sir Alexander announced
the Strontian mines as the most wonderful discovery of the age.
The miners built a town at the place which they called New York.
The only other point of interest about the history of the mines is
that strontia was first recognized as a distinct alkaline earth by
Crawford in 1790. Klaproth and Hope independently of him, and
of each other, investigated its properties in 1793.
The original mines are four in number, and are at a level of from
600 to 800 feet above the sea, They are all in Glen Strontian; their
names are Fee Donald, Bell’s Grove, Middle Shop, and Whitesmith.
Of these the three latter have been allowed almost entirely to fall in.
The only workings which have been carried on of late years have
been at Fee Donald and, to a slight extent, at Bell’s Grove. The
ore is Galena containing very little silver. At Fee Donald there is
a tradition of an antimony lode not now worked; and there is a
record of a steel-ore very rich in silver; but no specimens of either of
these are procurable.
The only minerals worth notice at Fee Donald are Calcite, espe-
cially Paper-spar, and Morvenite, the latter being rare.
At the other three mines minerals are very abundant; but unfor-
tunately it is impossible at present to ascertain from what levels they
are derived. The different species are almost entirely confined each
to its own mine, or rather to its own rubbish heap; for it is only in
these heaps that they occur.
At Bell’s Grove, Harmotome and Morvenite are extremely abun-
dant, the opaque variety of the mineral being the commoner. At
Middle Shop, Harmotome is not found, but Brewsterite appears either
on decomposing granite or on calcite. At Whitesmith the rubbish
heaps yield small fragments of Strontianite, associated with Brews-
terite, though I have never found the two minerals on the same spe-
cimen. The larger curved crystals of Brewsterite are usually on
Heavy Spar.
Whitesmith is by far the deepest of the mines, but it is also the
* highest up the side of the mountain.
There is nothing particularly new to be noticed about these mine-
* During a recent visit to Norway I found this type of gneiss to be very abun-
dant in that country, where it is known as “ eye-gneiss.”—Oct. 1871.
374 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
rals. As regards the general character of the gangue of the mine,
we are struck by the absence of Fluor, and the comparative rarity
of Blende and Heavy Spar. The last-named species we might fairly
expect to be present in considerable abundanee, as baryta is present
in such large quantity in the Harmetome and Brewsterite.
During the last six years anew mine, called Corrantee, has been
opened, at a distance of some two miles westward from Whitesmith, ©
but at the other side of the hill. It is, however, apparently on the
same lode that is worked in Glen Strontian, but is situated entirely in
the gneiss. I first visited this mine in 1866, and noticed the pre-
sence of the barytic Zeolites. Since that time some very beautiful
specimens have been obtained from it, notably of Caleite, im the
form of scalenohedrons terminated by rhombohedrons, and coated
with Harmotome.
Among other specimens I found some crystals of Harmotome
closely resembling those from Andreasberg, in fact true Cross-stone.
These were irregularly distributed over a mass of very acute scale-
nohedrons of Calcite, and associated with minute hexagonal prisms
apparently terminated by a basal plane, and perfectly transparent.
When I first noticed these crystals I felt sure that I had discovered
a new locality for Brewsterite; but on testing the mineral in the
blowpipe I found that it did not swell up, and that it gave a simple
baryta-flame. The borax-test proved abundantly that it was a
Zeolite. These results made me suspect that it was only a new form
of Harmotome.
Not being myself able to analyze it, from want of time, I requested
my friend Dr. J. H. Reynolds, Keeper of the Minerals in the Royal
Dublin Society, to examine it.
He detected that the termination of the prisms is not a single plane, _
but consists of two planes inclined to each other at a very obtuse
angle.
He therefore broke up a large specimen, picked out carefully all
the crystals which exhibited this peculiar termination to the prisms,
and subjected them to analysis.
He only succeeded in obtaining 1°5 gramme of the mineral by this
method, a quantity quite insufficient for a complete analysis, inas-
much as, owing to the necessity of determining the alkalies, he was
obliged to decompose the mineral by acid, and therefore could not
ascertain the amount of water present.
The following Table gives the best analyses of Strontian Harmo-
tome which have as yet been published; and it will be seen how
closely Dr. Reynolds’s analysis agrees with them.
A. B. C. 1D)
SiO,......... 47:74 47-52 47-60 48-02
Ona 1568 1694 1639 17-42
Heo. ae Con 0°65
BalO eee _ 21-06 20°25 20:86 20:17
OalOn aren eae he gale, © oly renee trace
KOM 0-78 1-00 0°81 0-62
NaiO pin. eae 0:80: 1:09 0:74
WYO} es cniss 13°19 13:45 14-16 13:77 (water and loss).
99°76 100:25 101-21 100-00
1871.] SCOTI—ARGYLLSHIRE MINERALS. 375
Of these, A is by Damour; it is of Harmotome, the opaque va-
riety. B, by Rammelsberg, is probably of the same ; it is simply called
Harmotome from Strontian by him. C is by Damour; it is one of
two analyses of Morvenite, by which he established the identity of
Morvenite with Harmotome. JD is Dr. Reynolds’s analysis.
From this it appears that these crystals are a particularly pure form
of the mineral, being nearly perfectly free from alkalies; and they
certainly deserve a name, to the full as much as Thomson’s Morve-
nite does.
The only special interest which they possess is crystallographical.
In all the crystals of Harmotome figured by either Dufrénoy or Dana
the termination of the prisms is quadrifacial. Dufrénoy mentions
that occasionally a very obtuse quadrangular pyramid is found, simi-
lar to that which sometimes occurs in Anatase; and Descloiseaux,
in his recent paper* on the crystallography of the species, has deter-
mined the angle between the opposite faces of this pyramid to be
178° 20’. Dana gives in his last edition such a pyramid.
I have not myself been able to measure the angle between the
faces of the dihedral termination of the prisms which I now submit
to the Society ; it is an extremely obtuse one; and it seems probable
that they will ultimately turn out either to be two of the four faces
spoken of by Descloiseaux, or else the faces of the brachydome cor-
responding to that pyramid.
In conclusion I would only draw attention to the specimens which
T have brought down, as evidence that the neighbourhood of Strontian
is still almost as promising a field for the mineralogist as any in these
islands.
DIscusston.
Mr. W. W. Suyt mentioned the wonderful collection of minerals
from Strontian which had been brought to the Great Exhibition of
1851, which gave a most striking idea of the mineral riches of the
locality. The occurrence of such a series of different substances in
one locality in the granite was almost unparalleled, though in the
-Andreasberg mines, in clay slate, they were to some extent rivalled.
The features, however, differed in the two places, more silver and a
greater number of zeolites being present in the Hartz mines.
Mr. D. Forses observed that Harmotome occurred also at the
Kongsberg silver-mines in Norway, at a distance from granite. He
thought it remarkable that these crystals of peculiar form occurred
in the same spot and in connexion with crystals of the same sub-
stance but of the ordinary form.
Mr. Davis remarked that Celestine was also to be placed on the
list of the minerals from Strontian. Harmotome had been found in
the same form of double crystals at Bodenmais in Bavaria.
Mr. Scorr stated, in reply to a question from the Chairman, that.
the mineral had not been as yet optically examined, but that if he
could procure more of it he should be happy to place it at the dis—
* Ann. des Mines, 4th ser, tom. ix. p. 339.
376 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
posal of any gentlenian who would examine it. As regarded the
idea that Harmotome usually occurred near the surface, he could
give no information about the old mines, as they had been allowed
to fall in; but most certainly the new specimens from Corrantee
came from surface-workings.. He was very glad to learn from Mr.
Davis that Celestine had been found at the locality; and he felt
sure that careful search would double or treble the number of species
known to oceur there. With reference to what had fallen from
Prof. Smyth, he could fully corroborate his observations as to the
difference between the forms of Calcite associated with Harmotome
at Andreasberg, in the Hartz, and at Strontian. It was remarkable
that the general facies of the crystals of Calcite occurring at Cor-
rantee, where the lode was entirely in the gneiss, differed from that
usually observed in the old mines in Glen Strontian, which were
partly in the granite and partly in the gneiss.
3. The PROBABLE Oriern of Devostts of “Lozss ” in Nortu Cina and
Eastern Asta. By Tuomas W. Krnesuixt, Esq.
(Communicated by Prof. Huxley, F.R.S., V.P.G.S.)
Tue Baron F. von Richthofen, in an able and interesting Report* of
a journey undertaken under the auspices of the General Chamber of
Commerce at Shanghai, alludes to the enormous area covered by the
light-clay deposits of North China which he found at Chinkiang and
Nanking, on the Yangtsze, and throughout almost the entire area
of Honan and Shansi. Beyond the area mentioned by the Baron,
they seem to extend into Shantung, to cover a large portion of
Northern Anhwei, and, according to Pumpelli, to reach to North
Chihli and Mongolia. The formation appears to answer in a great
measure to the Kunkur formation of India, and in all probability
extends far into the elevated plains of Central Asia. The name of
“ Loess,” taken from the similar deposit in the valley of the Rhine,
has been applied by the Baron yon Richthofen to this formation ;
and to it as a distinctive name, independent of any theory as to its
formation, there does not seem any objection. So many different
opinions have been held as to the origin of the Loess of the Rhine,
that it is not surprising a similar difference should exist in regard
to the vastly more extensive deposit of Eastern Asia. The latter,
however, though almost identical in structure and composition with
the former, differs widely from it in position, inasmuch as it is by
no means confined to the valleys of the great rivers, but stretches
almost uninterruptedly over the raised tablelands of Central and
Northern China. Like the Rhine-Loess it contains a large per-
centage of earthy carbonates mixed with impalpable siliceous sand,
and the ordinary constituents of clay. There is little to be added to
* No. III. Report on the Provinces of Honan and Shansi, fol. Shanghai,
1870.
1871.] KINGSMILL— CHINESE ‘‘ LOESS.”’ 377
the Baron’s description of the deposit* more than to say that in
places the carbonates have segregated from the mass in nodules of
fantastic shapes, which show, from the vertical position of their
major axis, their subsequent origin. These nodules are of impor-
tance in a description of the mass, as, in the neighbourhood of Chin-
kiang at least, they seem to divide the whole formation into at
* The following is Baron von Richthofen’s description of the deposit, extracted
from the Report already cited (pp. 9, 10) :—
«‘The Loess is among the various substances which would commonly be called
loam, because it is earthy and has a brownish yellow colour. It can be rubbed
between the fingers to an impalpable powder, which disappears in the pores of
the skin, some grains of very fine sand only remaining. By mechanical de-
struction, such as is caused by cartwheels on a road, it is converted into true
loam. When in its original state it has a certain solidity, and is very porous,
and perforated throughout its mass by thin tubes, which ramify like roots of
grass and have evidently their origin in the former existence of roots. They
are incrusted with a film of carbonate of lime. Water, which forms pools on
loam, enters therefore into loess as into a sponge, and percolates it without in the
least converting it into a pulp or mud. The loess is everywhere full of organic
remains; but I have never seen any other but land-shells, bones of land-animals,
and the numberless impressions of roots of plants. It is not stratified, but has
a strong tendency to cleave along vertical planes; therefore, wherever a river
cuts into it, the loess abuts against it, or against its alluvial bottom-land, in ver-
tical cliffs, which are in places 500 feet high; above them the slopes recede gra-
dually in a series of terraces with perpendicular front faces. Where the river
reaches the foot of such a wall, the progress of destruction is rapid; the cliff
is undermined, and the Loess breaks off in vertical sheets, which tumble into the
stream, to be carried down by the water. . . . . The beds of the affluents
which join the river in these places are no less deeply cut into the Loess, and
ramify into its more eleyated portions like the roots of a tree, every small
branch a steep and narrow gulch. . . . . It gives habitation to millions of
human beings. . . . . They live in excavations made in the [precipitous
walls of] Loess.
“As regards the mode of origin of this formation, the Loess of China, like
that of Europe (where it exists on a comparatively small scale), has been sup-
posed to be a freshwater deposit. This supposition is erroneous as regards the
Loess of Northern China, because it extends equally over hills and valleys, and
does not contain freshwater shells. Others have therefore considered it as a
marine deposit. This view is more erroneous even than the former, because it
would presuppose the whole of Northern China to have been submerged at least
6000 feet beneath the level of the sea in a recent epoch, while there is abundant
evidence to prove that such has not been the case. Nor-can the theory, current
in Germany, that the Loess of that country was produced by glacial action, be
at all applied to the Loess of Northern China, from various obvious reasons too
lengthy to explain here. Unbiased observation leads irresistibly to the conclu-
sion that the Loess of China has been formed on dry land. The whole of that
vast country, which was covered by a continuous sheet of Loess before this had
undergone destruction, was one continuous prairie, probably of greater elevation
above the sea than the same region is now. The Loess is the residue of all in-
organic matter of numberless generations of plants that drew new supplies in-
cessantly from those substances which ascend in moisture and springs, carried
in solution to the surface. This slow accumulation of decayed matter was as-
sisted by the sand and dust deposited through infinite ages by winds. The
land-shells are distributed through the whole thickness of the Loess ; and their
state of preservation is so perfect that they must have lived on the spot where
we now find them. They certainly admit of no other explanation than that.
here hinted at, of the formation of the soil in which they are imbedded. The
bones of land animals and chiefly the roots of plants, which are all preserved in
their natural and original position, give corroborative evidence.”
378 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
least three successive beds, showing that, contrary to the Baron’s
idea, the mass is really stratified, though the uniform character of
its constituents and their extremely mobile nature have for the most
part effaced any decided marks of deposition.
To account for the origin of the formation, Baron von Richthofen
has started the extremely ingenious explanation that the beds of
the Chinese Loess have been formed on dry land, his principal
reasons for this assumption being that the beds contain remains of
land-shells and land-animals to the exclusion of marine or even, so
far as known, freshwater species, and that no depression of the
eastern portion of the continent is sufficiently recent to allow of their
deposition under the surface of the sea.
I shall deal with these objections in reverse order, and afterwards
state some reasons against the subaerial theory.
Evidence of late depression in North China.—First, the Baron
states that there is evidence to prove that the north of China has
not been submerged to the depth of 6000 feet within a recent geolo-
gical epoch. Without arguing as to the difficulty of proving a nega-
tive of this sort, I shall only state that to my mind there is abundant
evidence, irrespective of the Loess itself, to prove that China, as far
north as the Yellow River (beyond which my personal experience
does not extend), has since the commencement of the Tertiary period
been the scene of very considerable depression. Proofs of this, I
believe, are to be found in the upper Nanking sandstones and con-
glomerates and their succeeding rocks. ‘These sandstones, in almost
perfectly horizontal strata, stretch from the south of Nanking through
northern Anhwei as far at least as Ting-yuen-hien in the Fung-yang
prefecture, being especially characteristic at Luchow-fu, in the
centre of this district. The upper portion of these rocks I believe
to represent the Tatung gravels of Baron von Richthofen. These
Tatung gravels extend through the south-western portion of Anhwei,
forming in many localities the bed of the present valley of the Yang-
tsze, are seen in still greater development in Hupeh, as at Hwang-
chow.and Wuchang-hien, and probably reach as far west as Ichang,
at the foot of the gorges of the upper Yangtsze. I have met with
them myself at San-kia-tientsze, some thirty miles from Fung-yang-
fu, in the north-east of Anhwei province, where they form a bold
escarpment looking over what was at one time the Yellow Sea, but
now constitutes the alluvial plain of Kiang-peh. I do not know how
much further in either direction these beds extend ; and, besides, I
wish to confine myself to facts within my own observation. If local
conditions at Kiukiang on the Yangtsze are to be trusted, these gravels
pass upwards into the Kiukiang laterite, a deposit occupying likewise
a considerable area in Anhwei, Kiangsi, and Hupeh.
It seems improbable that these rocks, which extend over so large
a space, are otherwise than marine, though at present no fossils have
been collected in them. The bold escarpments of the hills on either
side of the Yangtsze occur in localities where it seems impossible to
ascribe them to fluvial action. They are much more suggestive of
ancient coast-lines. They are, besides, not confined to the valley of
1871.] KINGSMILL—CHINESE “‘ LOESS.” 379
the Yangtsze; the elevated sandstone plain of northern Anhweiis in
places defined by escarpments of the older mountain-chains, rising
abruptly from its surface. The traveller in this district is, in fact,
forced to the conclusion that he is passing over an ancient sea-
bottom, the mountain-masses of the older Devonian and Carboni-
ferous formations forming islands, rising in lines of irregular cliffs,
which from their indented outline betoken a long-continued period of
depression.
These rocks are succeeded by the Loess. Before its deposition
they seem to have been partially, though slightly, denuded, denoting
probably some change in the physical conditions of the adjoining
land.
What is true of the four provinces adjacent to the Yangtsze is
probably true, likewise, with regard to the others over which the
Loess extends. There was, at some time subsequent to the upheaval
and denudation of the Carboniferous and apparently Triassic rocks,
a period of considerable depression in, at least, Central China. The
deposition of the Loess probably marked its close.
I have assumed the age of the sandstones and gravels to be T'er-
tiary, principally from their position, overlying all the older rocks,
and because comparatively little denudation has occurred in either
them or the older rocks since their deposition. As stated above, the
evidence of fossils is as yet wanting; but we may hope to see it sup-
plied. The main fact of the depression antecedent to the deposition
of the Loess may be regarded, however, as proved.
Structure of the Loess.—The other argument adduced in support
of the subaerial theory, as stated above, is founded on the internal
evidence of the deposit. Baron von Richthofen holds that the Loess
is unstratified; this, so far as relates to the absence of apparent
layers of deposition, is true, as it is likewise of the Loess of the Rhine.
As in the latter, however, the beds of calcareous nodules point to an
apparent stratification of materials. In this respect, as in others to be
pointed out, it bears a close mechanical resemblance to chalk, though
in mineral composition very different from that rock. The occurrence
of land-shells and remains of land-animals is looked upon as a strong
proof in support of this theory. The fossil origin of these exuvie,
however, is more than doubtful. The Loess is perfectly pervious
to water; to use the Baron’s own words, “It is perforated through-
out its mass by thin tubes, which ramify like the roots of grass, and
have evidently their origin in the former existence of roots.” Asa
fact, streams seldom or never flow on the surface of the Loess; they
take by preference underground courses, or work for themselves
deep valleys, penetrating into the mass in all directions, like branches
from the stem of a tree. This mass has, besides, a tendency to
cleave in vertical planes, enabling thereby the smallest streams to
penetrate its mass; so readily, moreover, is it acted on by water, or
even by aqueous vapour, that I have in my possession specimens
which disintegrated in the moist air of a Shanghai summer, and
which have since rearranged themselves at the bottom of the drawer
in which they had been placed. ‘These facts render the presence of
380 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
terrestrial remains of easy explanation, without accepting the theory
of subaerial formation: a shell or other animal relic has only to drop
into a fissure or be carried down by a stream of water during a
flood; the soil around readily adapts itself to its shape, fills its inter-
stices, and, in fact, in a short time loses so completely all trace of
having been disturbed, that the shell or other substance becomes a
pseudo-fossil.. On the other hand, if the foreign substances were
really contemporaneous with the mass, they would most probably
be found constituting the centre of aggregation in the calcareous
nodules spoken of. I have broken open probably some hundreds of
these, and never found a trace of fossils. The Loess, as I have
suggested above, bears, in some respects, a mechanical resemblance
to chalk. These are the extreme fineness of the particles of which
it is composed, the presence of vertical tubes leading downwards
from the surface, and the occurrence of nodules like the “ pot-
stones” in the chalk, with their major axes vertical. The large
amount of carbonate of lime in its composition is also worthy of note
in the comparison. All these reasons seem to suggest a similar
origin for the two formations—namely, on the bed of a tranquil sea.
Baron von Richthofen (I believe rightly) rejects the theory of the
Loess being of freshwater origin, as requiring a freshwater lake of
such enormous proportions that we cannot believe in its existence
at any period. The shape of the older mountain-chains, and their
peculiar weathering, he argues, forbid the supposition of glacial
Bee (See my former paper, Quart. Journ. Geol. Soc. vol. xxv.
p. 137.)
Materials of the Loess—In stating some of my grounds for coming
to the conclusion that the Loess is a true marine formation, I have
incidentally mentioned many objections to its subaerial origin as
suggested by Baron von Richthofen. There are, however, others of
even stronger nature. Its chemical composition, consisting, as ib
does, mainly of silicates of alumina and of free silica in the con-
dition of impalpable sand, does not correspond with that of the in-
organic elements of plants growing on its surface. Granting, how-
ever, that the earthy carbonates and a portion of the silica could be
derived from such a source, whence could the plants themselves
derive these elements, but in turn from the soil on which they grew ?
Lime, potassa, magnesia, iron, and silica might, then, so long as the
plant had access to subjacent formations, or was supplied by springs
from below, have been deposited in a superficial layer; silica might
even, as suggested, have been conveyed by the medium of dust-
storms; but whence could the silicate of alumina be derived? <A
superficial layer not altogether dissimilar, might, as suggested, be
formed so long as the plants had access to subjacent rocks. Once,
however, removed from contact with them, these inorganic elements
of the plants could only be supplied from the soil itself. Rivers are
inadmissible, as their action would have been to disintegrate, not to
build up; springs, from the peculiarities of the formation, cannot
rise to its surface. There is, finally, wo known means by which
these inorganic matters could have been supplied from the atmo-~
1871.] KINGSMILL—CHINESE ‘‘ LOESS.”” 381
sphere. The layer formed by one generation of plants would, in
effect, have been absorbed by the next without any addition being
possible.
Dust-storms, however, have been suggested as a source of supply.
Unless these passed over deposits of the Loess itself, I know of no
other source for the necessary ingredients. Clay would not be
acted on by the wind; sand, of itself, would not suffice to form the
peculiar mixture of ingredients ; limestone rocks have never, to my
knowledge, been so disintegrated by the action of the atmosphere
as to become reduced to dust capable of being transported in the
manner suggested. The means are therefore utterly inadequate to
the end.
Easy removal of the Loess by rain.—There are, however, other
grounds of objection. Had the Loess been formed as dry land, there
is no reason why it should not only have utterly ceased to increase,
but should be actually undergoing a rapid destruction. There is evi-
dence sufficient to prove that its waste now is greater than at former
periods, owing to the ignorant destruction of the trees with which,
tradition states, it was once covered. This destruction has increased
the frequency and force of the annual floods; but as long as rain
fell or rivers ran, denudation of one sort or other must have been
going on. Denudation above the sea-level is, in fact, as necessary
an accompaniment of running water asis deposition below it. When
it is remembered how sensitive is the Loess to the slightest contact
with water, and that ever since the emergence of the Loess district
from the waves every stream within its limits must have been con-
tinually engaged in the work of denudation, the difficulty of accept-
ing the subaerial theory becomes a practical impossibility.
Marine origin of the Loess.—Rejecting, then, as untenable the
theories which would assign a glacial, freshwater, or subaerial origin
to this peculiar formation, little remains except to class it as marine.
As yet, except in its peculiar structure, such as its mechanical re-
semblances to chalk, an undoubted deep-sea formation, no internal
evidence has been discovered to guide us to this conclusion. Speci-
mens of the clay were sent by Mr. Pumpelli to the United States,
and examined microscopically by Mr. Edwards; except, however,
some small green crystals, pronounced not to be organic, nothing
peculiar presented itself. There are here no means of making mi-
croscopic examinations, and but few for scientific operations of any
kind ; inductions have therefore to be founded on what, under more
favourable circumstances, would be deemed insufficient proof, trust-
ing to subsequent rigid investigation to prove or disprove their truth.
The real origin of the Loess will probably be proved by the close
examination of its microscopic structure; but even this must be to
a certain extent taken in connexion with its external conditions, as
Microzoa may readily be of derivative origin.
Probable Geological relationships of the Loess.—The assumption of
a marine origin for the Loess of eastern Asia leads up to most im-
portant geological deductions. It extends, as has been stated above,
from the south of the Yangtsze, in the prefecture of Chinkiang, far into
382 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 26,
Mongolia in the north, and from Anhwei on the east to an unknown
distance west, in all probability far into Central Asia. It rises in por-
tions, as in Shansi and Mongolia, to a height of about 6000 feet over
the present sea-level, forming at that elevation a deposit upwards
of 1000 feet deep. At its southern extremity, in Kiangsu, it does not
at present rise more than about 200 feet, though apparent fragments
in the sides of the hills rise possibly to 400 feet. Over the raised
plain of Anhwei it has been greatly denuded, and probably to a
considerable extent rearranged. We must therefore believe in a
general depression of Eastern Asia, at least from the latitude of 30°
to 45° north and from 90° to 120° east longitude. This, however,
is not all: South China, though probably never entirely submerged
during the Tertiary epoch, shows in its valleys some traces of marine
deposits of that age. Cambodia and Siam, as well as Birmah, with
their fossil forests and beds of animal remains, have probably joined
in the downward movement. The Sewalik hills, in India, seem to
point to an elevation of some 6000 feet since the Miocene period. If
Captain Montgomerie’s pundit is to be believed, the plain of Lhasa,
upwards of 11,000 feet over the sea-level, tells a similar tale. It
may therefore be assumed that within the Tertiary epoch the whole
of eastern Asia underwent a movement of depression and subse-
quent elevation. At the point of greatest depression, North China
(except perhaps a few summits, such as the Ho-shan, in Shansi)
was under the level of the sea; South China formed a group of
deeply indented islands, representing the ancient boundary-chains
of the southern provinces. During the time of depression, while
land was still near, the Luchow sandstones and Tertiary gravels
were deposited ; afterwards, in the bed of a comparatively deep and
tranquil sea, and at a distance from shore sufficient to have allowed
all but the most impalpable particles to have already subsided, the
Loess beds were thrown down.
Sufficiently startling, however, as is this induction, we can by no
means stop there if we accept the premises. One of the most re-
markable features in the geology of the chain of islands which bound
on the west the great Pacific Ocean, is the enormous development of
sandstones and coal-beds, accompanied with conglomerates of various
sorts. Some of these beds, as at Takosima, near Nagasaki, in Japan,
and at Apes’ Hill, near Taiwan, in Formosa, are rich in fossil re-
mains; the coal-beds of Borneo are also known to have yielded
characteristic fossils. Beginning, then, with Borneo,—stretching
through the Philippine Islands,—continuing on through Formosa
and probably the Loochoo Islands,—occurring again in Kiushiu,
Niphon, and Yesso, in Japan, and extending as far as the coal-field
of Dui, in Saghalien, we find a series of beds of sandstone, coal, and
conglomerate agreeing generally in geological structure, and yielding,
at such distant spots as Borneo, Formosa, and Kiushiu, characteristic
fossils of apparently Mid-Tertiary age.
If we accept the submergence theory for Eastern Asia during this
period, we must look elsewhere than to the present continent for the
supply of materials for these very extensive deposits, as well as for
1871.] KINGSMILL—CHINESE “‘ LOESS.” 383
the forests which have nourished these by no means insignificant
coal-fields, whether we describe them by their horizontal or vertical
extension. The small island of Takosima, which contains in a
thickness of about 450 feet three beds of coal, averaging from 6 to
8 feet in thickness each, is an instance of the latter. The great
length of the chain, some 50 degrees of latitude, is sufficient proof
of the former.
The mechanical structure of the beds forces us to believe in the
near proximity of a continent during their deposition. Sandstones,
conglomerates, and coal itself may all be accepted as proofs of littoral
conditions. Shut out from the west, we must therefore turn to the
east as the probable source whence these beds derive their immediate
origin. In this surmise we have, however, other grounds of proba-
bility to argue from. Darwin’s theory of fringing coral-reefs mark-
ing a period of depression has long been accepted by many of the
most able of geologists. Assuming it as proved, we are almost of
necessity led to the belief in a great Pacific continent during com-
paratively recent geological time. If we assume that its depression
was coincident with the elevation of the remarkable volcanic chain
of the west Pacific islands, we may assume that these marked its
western shores. Along these shores the greatest Tertiary coal-field
in the world was deposited, while at a distance the finer sediment
of its streams was thrown down over Eastern Asia in the form of
Loess.
Geologists have been ready enough to accept great depressions
during the Tertiary epoch, but have hitherto hesitated in pointing
out the necessary counterbalance which must have existed between
the areas occupied by land and water. I have therefore, at the risk
even of being thought to a certain extent an innovator in the science,
pointed out a few of the facts which have influenced me in placing
the counterbalance within the limits now occupied by the Pacific
Ocean.
Discussion.
Prof. Ramsay remarked that the author had not proved that the
’ Loess he described was really stratified. He could not agree with
his views of the inland escarpments he mentioned having been old
coast lines. It was only accidentally that sea cliffs had any con-
nexion with the line of strike of the strata, whereas inland cliffs
always followed the strike. He thought the phenomena were rather
in accordance with a long exposure of the land to subaerial in-
fluences than with the Loess having been of marine origin. Even in
England, in those parts which had long been free from marine
action, beds of brick-earth had been formed. He also instanced the
plains of Picardy as exhibiting a vast extent of such subaerial beds.
Prof. T. Ruvert Jones thought that the area treated of by Mr.
Kingsmill was too large to have its geology explained merely by re-
ference to rain-wash and valley deposits. Whatever his low-level
Loess might be, the higher accumulations of loamy deposits, stated
to be 1000 feet thick at an elevation of 3000 feet, and regarded by
384 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
Mr. Kingsmill as the quiet water sediments of a great gulf with the
Miocene conglomerates and sandstones of Nanking and elsewhere
for its marginal equivalents, appeared to require a different expla-
nation. All loess need not be of river origin ; in oscillations of land
marine deposits must be carried up to great heights; and, referring
to Mr. H. M. Jenkins’s determination of the marine origin of the
Loess of Belgium, Prof. Jones thought it highly probable that some
at least of that in China may have been similarly formed.
Mr. Huenus said that the author appeared to have grouped to-
gether all the superficial deposits of a vast area without explaining
very clearly the grounds upon which he identified those deposits at
distant points. He did not prove that what he called the shore de-
posit was marine, or that it was of the same age as the loam which
he described, and which Mr. Hughes thought, from the description,
was far more likely to be subaerial.
Mr. Evans and Mr. Ernzriper suggested the probability of much
of the so-called Loess having been brought down from higher loamy
beds, possibly derived from the decomposition of limestone rocks
containing sand and clay, and redeposited by the action of rain.
May 10, 1871.
Dr. Henry Nyst, of Brussels, was elected a Foreign Member, and
Prof. G. Dewalque, of Liége, a Foreign Correspondent of the
Society.
The following communications were read :—
1. On the Anctunt Rocks of the St. Davin’s Promontory, SouTH
Wares, and their Foss1z Contents. By Professor R. Harxyass,
F.R.S., F.G.S., and Henry Hicks, Esq. With Descriptions of the
New Species, by H. Hicxs, Esq.
(Puates XV. & XVI.)
In an early edition of Siluria (1854) there is a figure of a specimen
of Paradoxides Forchhammeri? Angel., from the black slates of North
Wales. In the third edition of the same work (1859) the same
figure occurs, with the remark “locality unknown, probably from
Pen Morfa, near Tremadoc, North Wales.” In this edition there
is also a note with reference to the occurrence of this form, stating
that “only one species of Paradowides has yet been found in Wales ;
although the specimen is imperfect, Mr. Salter believes it to be iden-
tical with P. Forchhammert of the alum slates of Andrarum in
Seania.”
In the last edition of Siluria (1867) the same figure is named
Paradowides Hicksti; its locality is indicated as “‘near Dolgelly,
North Wales ;” and it is further stated that “this fossil has been
1871.] HARKNESS AND HICKS—ST. DAVID’S PROMONTORY. 385
found both at Dolgelly and in Pembrokeshire, about a hundred feet
above the lowest black Lingula-slates.”
Respecting the discovery of another form, Paradowxides Davidis,
Salter, in Pembrokeshire, the late Mr. Salter has described this
species, and named the locality whence it has been obtained*.
In this memoir a Table is also given of the strata which make up
the “ Lingula-flags in Wales;” and Mr. Salter has described the
lower portion of this series as a ‘thick mass of black shales very
uniform in its upper part, but with hard sandstones in the lower,
probably accumulated in a deep sea.” The fossils of the Lower Lin-
gula-flags are stated to be “ Lingulella, rare, Olenus, common, Ag-
nostus, common, Paradoxides Davidis”’ *.
Subsequently Mr. Salter, in a communication entitled “‘ On some
New Fossils from the Lingula-flags of Wales,” described and figured
several new forms of Trilobites, a Theca, and a large Sponge ob-
tained from the dark-coloured rocks of Porth-y-Rhaw by Mr.
Hicks ¢.
In this memoir a section is given of the fossiliferous rocks, show-
ing their relation to the purple and green sandstones on which they
repose.
In 1865 Mr. Salter alludes to the occurrence of ‘‘ Some additional
Fossils from the Lingula-flags;” and a note on the genus Ano-
polenus is appended to this communication by Mr. Hicks§. The
lower portion of these Lingula-flags affording the additional fossils,
and also those previously referred to, were designated by Messrs.
Salter and Hicks, in a paper read at the British Association in 1865,
the “‘ Menevian group.”
In 1867 a new form of Lingulella (L. ferruginea, Salter), from the
Lower Lingula-flags of St. David’s, was described ; and the occurrence
of a variety of the same, Lingulella ferruginea, var. ovalis, Hicks,
which had been obtained from the underlying red rocks, was al-
luded to ||.
In this communication of Messrs. Salter and Hicks we have the
first indication of the presence of fossils in the purple and green
rocks of the St. David’s promontory, upon which the Lower Lingula-
flags are superposed.
In 1868 Messrs. Salter and Hicks gave an abstract having refer-
ence to the occurrence of some new fossils from the Menevian group
(Lower Lingula-fiags); and in 1869 a detailed description was
given of these fossils J.
The discovery of fossils in the dark-coloured Lower Lingula-flags
* Quart. Journ. Geol. Soc. vol. xix. p. 275.
+ This description of the Lower Lingula-flags was correct so far as then
recognized in North Wales ; but it does not include that very important portion
at the base, which has since been separated by Messrs. Salter and Hicks, and
named the Menevian group. Paradoxides Davidis belongs to this group, and
should not be associated with Olenus, the typical genus of the Lingula-flags
roper.
: : Op. cit. supra, vol. xx. p. 233. § Op. cit. supra, vol. xxi. p. 477.
| Op. ett. supra, vol. xxiii. p. 339.
q Op. cit. supra, vol. xxiv. p. 519, and xxv. p. 51.
VOL. XXVII.—PART I. 25
386 © PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
of Pembrokeshire by Mr. Hicks induced other geologists to seek for
similar fossils among the equivalents of these rocks in connexion with
the Lower Lingula-flags, which repose conformably upon the upper
portion of the purple rocks forming the Merionethshire anticlinal.
In reference to the rocks which rest upon the purple strata on the
east side of this anticlinal, Mr. Plant communicated a memoir en-
titled ‘‘ Notes relating to the Discovery of Primordial Fossils in the
Lingula-flags in the neighbourhood of Tyddyngwladi’s Silver-lead
Mine.” An abstract of this was published in the Quart. Journal of
the Geol. Soc. in 1866 ; and the memoir appeared im eatenso in the
Trans. of the Geol. Soc. of Manchester. A list of fossils obtained
from the Lower Lingula-flags of this portion of Merionethshire was
given by Mr. Plant; and this list exhibits a series having a very
intimate relation with that containing the fossils obtamed by Mr.
Hicks from Porth-y-Rhaw, near St. Dayid’s.
The Lower Lingula-flags of the valley of the Mawddach, Merio-
nethshire, are seen occurring between hard dark-grey shale-beds,
which afford Oleni, and the highest member of the purple rocks of
the anticlinal; and the Lower Lingula-flags here are conformable
to the deposits above and below them. In their mineral nature they
have great affinity to their equivalents near St. David's, consisting
of what Mr. Salter termed “sandstones probably accumulated in
deep water.’
The strata at Porth-y-Rhaw, which are rich in Trilobites, contain.
no red or purple rocks associated with them, but are grey in colour
at their base, being banded by light and dark shades, and black in
their upper portion; and it is in the latter that fossils are most
abundant.
Beneath the grey beds, and having the same inclination as the
Lower Lingula-flags (Menevians) there is, in the St. Dayid’s pro-
montory, a great development of rocks, which exhibit red, purple,
green, and greenish-grey colours. These rest upon a conglomerate
composed of quartz pebbles, of various sizes, cemented together by a
reddish or purple sandy matrix.
The beds upon which the conglomerates rest are greenish in colour,
and these are supported by rocks of rather peculiar characters.
In many spots they have an aspect which so nearly resembles
syenite that it is, at first sight, very difficult to make out their true
nature ; for they appear to be made up of crystals imbedded in a base
of quartz. When, however, these apparent crystals are carefully
examined, they are found to be, for the most part, angular frag-
ments of quartz, not possessing the proper crystalline form which
this mineral assumes. Some of the fragments have a subangular
outline; and a few even manifest a distinctly rounded surface. The
matrix in which these fragments are imbedded does not exhibit a
crystalline arrangement, and contains a very large proportion of
silica as a constituent. The chemical composition of a specimen of
these rocks has been kindly determined by Dr. Blyth, of Queen’s
College, Cork, and is as follows :— .
1871.] HARKNESS AND HICKS—6T. DAVID’S PROMONTORY. 387
Silicagsn Hee ensste nee e eerie ceinnssenenerwesie 78
Alliinniiaga seen epee Cees aol donee 16:5
Mime. soda-an Gd yironue see eet neeeereee eee ee 5-5
100
The proportion of silica afforded by the foregoing analysis much
exceeds that which is obtained from rocks having a syenitic nature.
These quartziferous rocks form an H.N.E. and W.S.W. course ;
and near the centre of this ridge is the city of St. David’s.
The arrangement of these rocks, which seem to be quartziferous
breccias, is rather indistinct. In the immediate neighbourhood of St.
Davyid’s, and also near Clegyr Bridge, about a mile E. from St.
David’s, they have associated with them irregular bands of hard
greenish-coloured ashy-looking shales, considerably altered in cha-
racter, but in many instances possessing distinct traces of foliation.
Bands of this shale have also been met with in well-sinkings in St.
David’s*.
Differences prevail in the characters of the rocks which repose
upon the central ridge, those on the S.8.E. side presenting an aspect
somewhat different from those on the opposite side. This difference
seems to have resulted from faults which have brought various rocks
of the purple and green series into contact with the quartziferous
breccias.
The quartziferous breccias on the 8.8.E. have, for the most part,
resting upon them quartz rocks of a greenish-grey colour and
compact nature. These possess many of the features of horn-
stone, and they are intersected by closely approximated joints.
They have, however, a distinct 8.8.E. dip at a high angle, usually
about 80°; and in this position they are well seen in the neigh-
bourhood of Clegyr Bridge, where their strike is parallel to the
axis of the quartziferous breccias.
On following the line of strike of the hornstones for a short
distance towards the W.S.W., these rocks are found to disappear.
At the ruins of Nun’s Chapel, about a mile W.S.W. from Clegyr
Bridge, the compact quartz rocks are seen; but immediately beyond
this all traces of them are lost, and a greenish flaggy sandstone
appears at Porth Clais Harbour resting against the quartziferous
breccias.
The connexion between the quartziferous breccias and the greenish
flagey sandstones at Porth Clais Harbour results from a fault, having
a throw-down on the E.S8.E. side, by means of which rocks newer
than the compact quartz rocks, or hornstones, are brought into con-
tact with the quartziferoys breccias. At Porthlisky, a little to the
* Since this paper was read, I have been fortunate enough to find two or three
spots in the ridge where the bedding is distinctly shown, and where the shales
are seen alternating with the more massive quartziferous beds. The strike of
the beds is from N.W. to 8.E., and hence quite discordant to the overlying
Cambrian series, in which the strike is from N.E. to S.W. ‘This ridge, there-
fore, must represent a more ancient group of rocks than the Cambrian, oc-
cupying a position equivalent to that of the Laurentian group in Canada.—
H. Hicxs.
252
388
(Corrected by Mr. Hicks, September 1871.)
Fig. 1.—Section across the St. David’s Promontory.
W.N.W.
E.S.E.
Porth-y-
Rhaw.
Fault.
Clegyr
Welle
St. David’s
Valley.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
d. Lingula-flags.
e. Trap.
The dotted Cambrian beds are conglomerates.
Cambrian altered.
c. Menevian.
b!.
* Beds which have yielded fossils.
6. Cambrian (Longmynd).
a. Laurentian.
W. of Porth Clais, purple sand-
stones, which will be shown to be
higher in the series than the green-
ish flaggy rocks, strike against the
quartziferous breccias, affording
further evidence of the occur-
rence of a fault in this neighbour-
hood.
It has been stated that at the
ruins of Nun’s Chapel the compact
quartz rocks are in connexion with
the quartziferous breccias.
At this locality there are seen
resting, apparently conformably,
on the compact quartz rocks, con-
glomerates already referred to as
being composed of large and well-
rounded masses of quartz imbedded
in a purple matrix. These conglo-
merates, as here seen, are about
30 feet in thickness.
The same conglomerates are well
shown near Clegyr Bridge, where
they appear to be conformable to
the underlying compact quartz
rocks, their dip being towards the
8.8.E., at about 80°. In this lo-
cality the thickness of the con-
glomerates amounts to about 60
feet.
On the N.N.W. side of the axis
of the quartziferous breccias no
compact quartz rocks are recog-
nizable; but some fine-grained
yellowish beds of a soft and de-
composing nature are seen in con-
tact with the quartziferous brec-
cias, and are succeeded by purple
conglomerates.
The section on the 8.8.E. side of
the axis exhibits a good develop-
ment of greenish flaggy sandstones
identical with those alluded to as
occurring at Porth Clais Harbour ;
and these sandstones are confor-
mable to the conglomerates on
which they rest. The greenish
flaggy sandstones have been
worked, especially at Caerfai;
and a small quarry of them is also
1871.] . HARKNESS AND HICKS—ST. DAVID’s PROMONTORY. 389
seen on the EH. side of the stream below Clegyr Bridge. These rocks
have a thickness of about 400 feet ; and on the N.N.W. side of the
axis the greenish flaggy sandstones also occur, resting conformably
on the conglomerates.
On the 8.8.E. side of the ridge the greenish flaggy sandstones
have above them red shaly beds, agreeing in their inclination with
the strata on which they repose; and these red shaly beds have
afforded the earliest traces of organic remains which have been
hitherto discovered in the St. David’s promontory. These remains
consist of Lingula ferruginea, Salt., a form previously mentioned,
another and larger Lingulella, a Discina, and a new species of Le-
perditia of considerable size, L. cambrensis, Hicks.
These red shales occur on both sides of the quartziferous ridge.
They are seen on the N.N.W. side, in Ramsay Sound, where fossils
have also been obtained from them near Castell. A small frag-
ment of a Trilobite has likewise been met with in the red shales of
this locality ; but this fragment was not sufficiently distinct to allow
of the form being satisfactorily determined.
On the 8.8.E. side of the ridge the fossiliferous shales are seen
at Porth Clais Harbour ; and in this spot also fossils occur*. They
are likewise seen under the ruins of Nun’s Chapel, at Rhoscarry-
Ihuyd, and also at Caerfai and Mill. These red fossiliferous shales
have a thickness of about 50 feet.
On the 8.8.E. side of the axis, reposing conformably on the
fossiliferous red shales, purple sandstones having occasional green
bands associated in them occur, somewhat coarse in grain. These
purple sandstones are about 1000 feet thick; and hitherto no fossils
have been obtained from them. These sandstones are now being
largely worked, the stone used in the restoration of the Cathedral
of St. David’s being obtained from them. They afford large blocks,
which dress well.
On the N.N.W. side of the axis the thick purple sandstones are
represented by deposits having more varied colours. On the KE. side
of Ramsay Sound, where the fossiliferous red shales occur, these
are seen to be succeeded by greenish sandstones, upon which are
rocks reddish in colour passing upwards into a series of purple strata.
Greenish sandstones rest upon the purple strata; and above these
are purple-coloured beds, having within them red layers. These
varied-coloured sandstones represent the thick purple sandstones on
the 8.8.E. side of the axis; and they are also almost unfossiliferous,
so far as present observations go.
The thick purple sandstones of the 8.8.E. side of the St. David’s
promontory have superposed conformably upon them yellowish- and
erey-coloured sandstones and shales. In the lower portion of these
yellow-coloured rocks there have been found remains of a large and
new form of sponge, Protospongia major, Hicks. ‘These strata,
which have some conglomerate beds associated with them, have
also afforded Trilobites, one of which appertains to a new genus, and
the other forms are new species. These are Plutonia Sedgwicki,
* Davidson on the Harliest British Brachiopoda, Geol. Mag. vol. v. p. 306.
390 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
Hicks, Conocoryphe Lyelliz, Hicks, Microdiscus sculptus, Hicks, Ag-
nostus cambrensis, Hicks, Protospongia fenestrata, Salter, Theca an-
tiqua, Hicks, and Paradoaides Harknessi, Hicks.
The yellowish-coloured sandstones and shales are well seen on
their line of strike in most of the headlands which intervene between
Porth Clais Harbour and Caer-bwdy. The principal spot from
which fossils have been obtained is the second headland EK. of Porth
Clais Harbour. The same rocks can be seen also between Folly and
Trelerwr. Their thickness amounts to about 150 feet; and on the
N.N.W. side of the axis their equivalents occur in a nearly allied
form, being yellowish-grey sandstones.
Succeeding these are grey rocks with purple bands, which pass
upwards into purple and red sandstones and shales ; and from these
Lingulella ferruginea, var. ovalis, Conocoryphe solvensis, Paradoxides
Harknessi, aud several of the other species have been obtained be-
tween Solva and Whitchurch. ‘The total thickness of the two series
on the 8.8.E. side of the axis is about 700 feet. On this side of the
axis these rocks are intersected by lines of faults, which run parallel
to their strike; and one of these extends from the coast a little 8.
of Folly through Trelerwr. These faults have downthrows on their
S.S.E. side, which have reduced very materially the absolute thick-
ness of those rocks on this side the promontory.
On the EK. side of Ramsay Sound, and on the N.N.W. side of the
axis, the equivalents of the grey and purple sandstones do not seem
to have been affected by faults; and here they have a thickness of
about 1500 feet.
On this side of the ridge also the grey and purple sandstones have
their representatives in “the form of grey, purple, and red flaggy
beds.
On the S.8.K. side the grey and purple sandstones have, resting
conformably upon them, grey grits, which contain Paradoxides
aurora, Salter, and Conocoryphe bufo, Hicks; and these two forms
have not, up to the present time, been discovered in strata which
underlie or overlie the grey grits. Agnostus cambrensis and Theca
antiqua have also been obtained from these grey beds. These two
species also occur in the underlying rocks; but they have not yet
been met with in deposits higher than the grey grits. Discina pi-
leolus, Hicks, and Obolella sa gutalis, Salter, are also found in the
grey beds. They likewise occur in the underlying purple strata, and
they extend upwards through the Menevian group.
Lningulella ferruginec is also found in the grey beds; and this form
has the widest range of any of the fossils that have been obtained
from the purple and green rocks of the St. David’s promontory. It
occurs in the lowest fossiliferous zone which has hitherto been dis-
covered, and it extends through the Menevians. Theca penultima,
Hicks, also occurs in these grey rocks; and this is the lowest
horizon from which it has been procured. Its range seems limited,
as it has not been met with above the lower portion of the Mene-
vilans.
On the N.N.W. side of the axis, on the HE. shore of Ramsay
1871.] HARKNESS AND HICKS—ST. DAVID’8 PROMONTORY. 391
Sound, these grey fossiliferous grits are not seen: a fault having
an H.N.E. course has cut through the upper portion of the purplo-
coloured rocks which support the grey strata. A few beds of theso
grey grits, however, are seen on the N.N.W. side of this fault, near
Ogaf Golhfa, in Whitesand Bay, reposing upon the higher members
of the purple flags and sandstones. ‘The order of the rocks from the
quartziferous breccias upwards, when not disturbed by faults, is as
follows :—
Lower Cambrian.
feet.
1. Greenish hornstones on the S.E., and earthy greenstones on the N.W..,
forming the outermost portions of the so-called Syenitic and Green-
stone ridges.
2. Conglomerates composed chiefly of well-rounded masses of quartz im-
peddedsimvaypunale maa brine eses eee eetct <eeeconseecece eres seen cue ce 60
So Greenish Hag ey, SANASTOMES)..c..c0n seein cll eisetecy cocaebeceeceereneceisesncess 460
4. Red flaggy or shaly beds, affording the earliest traces of organic re-
mains in the St. David’s Promontory—namely, Lingulella ferruginea,
Leperditia cambrensis, a larger Lingulella, and a Discind...........++ : 50
5. Purple (sometimes greenish) sandstones ...00....sceseeeeeecseseeeesseseeeee 1000
6. Yellowish-grey sandstones, shales, and flags containing the genera
Plutonia, Conocoryphe, Microdiscus, Agnostus, Theca, Protospongia,
SAIC ACCOM CS omen aucanatccweinens se tice atnsuetiaseunenicuses ‘eas tane sees 150
7. Grey, purple, and red flagey sandstones, containing most of the above-
TONEY TOTNES | MASSE) Gaconadunbnccsecobneoanceceogs seconneda CooGenHnaGooKEROsOb05006 1500
8. Grey flagey beds, containing Paradoxides Gurord...........ceee.eseees seen 150
9. The true beds of the ‘‘Menevian Group,” richly fossiliferous, and the
probable equivalents of the lowest portions of the Primordial Zone
OIE IM Lo IB RIS INE ES tooo Sanaa soe deponcnonade rsd docs oocendceduedouneaqoanbnbencar 550
The discovery of a fauna specially rich in Trilobites among the
purple and green rocks and their associated strata of the St. David’s
promontory affords very important information concerning the earlier
forms of life which occur in the old sedimentary deposits of the British
Isles. Until the discovery of this fauna, these rocks and their equi-
valents in North Wales have been looked upon as all but barren in
fossils. We have now scattered through about 3000 feet of purple
and green strata a well-marked series of fossils such as have nowhere
else been obtained in the British Isles.
In the Longmynds of Shropshire, consisting of purple and green
rocks, which probably represent the rocks having the same colour
in the St. David’s district, the only evidence of the existence of
life during the period of their deposition is in the form of worm-
burrows—and in the somewhat indistinct impressions which Mr.
Salter regarded as trilobitic, and to which he has given the name
Paleopyge Ramsayi*.
If we assume the purple and green shales and sandstones with
their associated quartz rocks of Bray Head, and the drab shales of
Carrick McReily, co. Wicklow, to represent the old rocks of the St.
David’s promontory, they afford only very meagre evidence of the
occurrence of life during the period of their deposition, in the form
of worm-burrows and tracks and in the very indeterminate fossils
which have been referred to the genus Oldhamia.
* Quart. Journ. Geol. Soc. vol. xii. p. 249.
392 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [May 10,
There is one very prominent feature about the paleontology of
the ancient rocks of St. David’s: this is the occurrence of four dis-
tinct species of the genus Paradowides; and this feature contrasts
very strongly with the entire absence of the genus Olenus from these
rocks.
On a comparison of the paleontology of the St. David’s rocks
with those of the continent of Kurope and of America, which seem
to occupy nearly the same horizon, we have like features, to a very
great extent, presenting themselves.
The lower fossiliferous horizon of Sweden, the Alum-shales, has
been divided by Angelin into two groups. The lowest of these,
“Regio B,” contains forms of Paradoxides, among which we learn
that Dr. Otto Torell has recognized two species that are St.-David’s
forms, viz. P. Davidis and P. Hicksti. The upper portion of the
Alum-shales of Sweden, ‘‘ Regio A” of Angelin, contains several forms
of Olent; and from this portion of the series the genus Paradoaides
seems to be absent.
The deposits upon which the Alum-shales of Sweden rest, the
“Fucoidal Sandstones,” contain within them purple beds; and
from these we have reason to believe that evidence of life has been
obtained by Dr. Otto Torell in the form of an Obolella. Tn Sweden
the genus Paradowides is found accompanied by Conocoryphe (Cono-
ccphalites) ; and Trilobites of this genus are also found associated
with Paradowides in the St. David’s promontory.
Regio B of Angelin is represented by the dark-coloured rocks of
Porth-y-Rhaw ; and below these are strata which seem to be the
equivalents of the Fucoidal Sandstones of Sweden, yielding an ex-
tensive series of fossils.
In N. Wales, on the E. and N.E. side of the Merionethshire
anticlinal, Regio B is also represented, and is succeeded by the
equivalents of Regio A, which, in the form of a thick series of
dark-coloured sandstones and shales (Lingula-flags), contain several
species of the genus Olenus.
In Bohemia, the primordial zone of Barrande, as shown by its
fossil contents, is very near to the horizon of the Menevian group as
exhibited in Wales. Trilobites appertaining to the genera Para-
doxules, Conocoryphe, Ellipsocephalus, Sao, and Agnostus occur ;
but no traces of the genus Olenus have been obtained from the
Bohemian primordial rocks.
In Bavaria, Sir R. I. Murchison states that, in the neighbourhood
of Hof, the primordial zone, “ which consists of black siliceous slate,
above 50 feet thick, contains Trilobites, which have been determined
by Barrande to belong to Conocoryphe and Olenus ;” and in a letter
from M. Barrande to Sir Roderick it is said that “with these pri-
mordial Trilobites are also associated two or three forms which every-
where characterize the second Silurian fauna (Llandeilo and Caradoc),
i.e. Calymene and Cheirurus”*,
With reference to the fauna of the primordial zone of Hof, Bar-
rande has remarked on the absence of the genus Paradowides there-
* Quart. Journ, Geol. Soc. vol. xix. p. 362; Siluria, 4th edit. p. 574.
LS 72F| HARKNESS AND HICKS—ST. DAVID’S PROMONTORY. 393
from. He regards the fossils which occur in these primordial rocks
as being of a later age than those found in the primordial zone of
Bohemia ; and he looks upon them as representing a period between
the first and second faunas of Bohemia *.
This fauna of Hof has no analogy with the ancient fauna of the
St. David’s promontcry. It is altogether much higher in position,
and connects the upper portion of the Lingula-flags of Wales, not
only with the succeeding Tremadoce rocks, but also with higher mem-
bers of the Silurian series.
The occurrence of rocks which appertain to the primordial zone of
Barrande, in Spain, has been referred to by Sir R. I. Murchison +.
The arrangement of these Spanish representatives of the primor-
dial zone has been given in detail by M. Casiano de Prado ¢.
The fauna of the Spanish primordial rocks, which has been ob-
tained from a thin series of red limestones, has been described by
Barrande. Among the fossils which it affords are seven Trilobites,
referable to the genera Paradoaides, Arionellus, Cenocephalites, and
Agnostus. The genus Paradowxides is represented by P. pradoanus,
a form which seems to occur only in Spain. The species of Ario-
nellus is A. ceticephalus, Barr., which is a form found in the primordial
rocks of Bohemia. There are three species of Conocephalites among the
Spanish representatives of the primordial zone, of which two are Bo-
hemian, viz. C. coronatus and C. Sulzeri; and one form, C. Ribeiro,
Barr., has not yet been obtained elsewhere. Two species of the
genus Agnostus are also met with in the Spanish primordial rocks,
These several Trilobites have been obtained from deposits which lie
north of Scabero, and of Bonar, in the province of Leon.
Sir R. I. Murchison also states that MM. de Verneuil and Louis
Lartet have discovered a “primordial” Silurian range with the
same species of Trilobites near Daroca. They also found it in
various parts of the Silurian strata which extend from Daroca to
Moncayo §.
The occurrence of fossils, of a type allied to those which are ob-
tained from the rocks of St. David’s, has been recognized in several
localities in North America. Mr. Salter has mentioned Paradowxides
Harlani, Green, as occurring in great quantities in Massachusetts.
P. Bennetti, Salter, is found in hard, fine-grained, flinty shales at
Branch, in the promontory between St. Mary’s and Placentia Bays,
Newfoundland ; and Mr. Salter alludes to the occurrence of Conoce-
phalites antiquatus, Salter, as a form which was exhibited at the
Great Exhibition, 1851, and which was obtained from a boulder of
brown sandstone in Georgia ||.
Dr. Dale Owen has mentioned the occurrence in Wisconsin of
several forms of Dikelocephalus, with species of Conocephalites, Ari-
* Faune Silurienne des Environs de Hof, December 1868.
+ Siluria, 4th edit. p. 416.
t Bull. Soe. Géol. France, 1860, vol. xvii. p. 516 e¢ seg.
§ Siluria, 4th edit. p. 416.
|| “Fossils of the Lingula-flags or Primordial Zone,” Quart. Journ. Geol.
Soc. vol. xv. p. d51 ef seq.
394 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
onellus, and Lonchocephalus, in the equivalents of the Potsdam sand-
stone. The genus Paradoxides however, does not, scem to be
represented in this fauna *.
A species of Paradoaides, which appears to be identical with a
form occurring in Bohemia and Thuringia, P. spinosus, Boeck, has
been met with in altered argillaceous sandstones in a quarry in Quincy,
south of Boston, in eastern Massachusetts +.
In Canada, at Point Lévis, on the banks of the St. Lawrence, a
fauna, possessing a character nearly allied to that mentioned by Dr.
D. Owen as occurring in Wisconsin, is seen. Among the thirty-six
forms of Crustacea which this fauna affords are two forms of Ario-
nellus, one of Conocephalites, and five of Dikelocephalus. These are
associated with fifty-five species of Mollusca, four of Radiata, and
forty-two forms of Graptolites, the latter being generically and, in
most instances, specifically identical with those of the Skiddaw
slates +.
The fossils of Point Lévis occur in limestone conglomerates and
in interstratified slates. These rocks appertain to the Quebec
group, and represent in this part of North America the calciferous
sand-rock §.
In Vermont, as seen at Swanton Falls, the Potsdam sandstones are
exhibited in the form of dolomites and red sand-rocks. The lower
portion ef these afford Conocephalites Adamsi, Bill.; and from the
higher strata C. Tenert, Bill., Paradoxides Thompsoni, Hall, P. ver-
montiana, Hall, and three species of brachiopods are obtained ||.
Strata of the same age, and affording the same forms of Paradowides,
oceur on the coast of Labrador, on the north-west side of the
Straits of Belle Isle. Here Conocephalites, with two forms of Ba-
thycirus, three of Salteria, and several brachiopods are found asso-
ciated 4.
The Potsdam sandstones are represented in the north-west portion
of Newfoundland. The strata here, which have been termed by the
late Mr. Jukes the Lower Slate formation, consist of the Signal-hill
sandstones and the St. John’s slate (Report on the Geology of New-
foundland).
From the slates on the west side of St. Mary’s Bay Mr. C.
Bennett obtained Paradoxides Bennetti, Salter, a form before al-
luded to.
Dr. Dawson refers to the occurrence of a rich primordial fauna in
New Brunswick. It affords fourteen species of Conocephalites, two
of Paradowxides, one of Microdiscus, and two of Agnostus, associated
with six forms of Brachiopoda **.
* Geology of Wisconsin, vol. i. p. 72.
+ H. D. Rogers, Geol. of Pennsylvania, vol. ii. pl. 11, p. 816.
{ Sir W. E. Logan’s Report on the Geology of Canada, 1863, p. 232.
§ Professor Dana, in the last edition of the ‘Manual of American Geology’
(1870), p. 171, unites the Potsdam sandstone and the calciferous sand-rock into
one group, placing them at the base of the Silurian, and designating the epoch of
their deposition as the ‘‘ Potsdam or primordial period.”
|| Report, p. 811. q Report, p. 866.
** Acadian Geology, 2nd edit. p. 641.
187 1.] HARKNESS AND HICKS—ST. DAVID’S PROMONTORY. 395
With reference to the distribution in time of the earlier genera of
Trilobites, it would appear that the genus Olenus is represented in Bri-
tain and Europe by twenty species, which are confined to the horizon
of the Lingula-flags, but not occurring so low as the Menevian group,
and by two species which, in Wales, are found in the higher horizon
of the Tremadoe slates. In America there are four forms of this
genus, and these are found in positions higher than any of the Old-
World species ; and the American forms are distinct from those of
Britain and Sweden. ‘Three of these species occur in the Quebec
series; and one O. undulostriatus, Hall, has been obtained from the
Hudson-river group.
Of the genus Conocoryphe (Conocephalites) there appear to have
been found in the Potsdam sandstone of America twenty-six species ;
and if to them we add the fourteen forms obtained by Dr. Dawson
from New Brunswick, forty species of this genus seem to occur in
the New World, all being low down in the primordial rocks. There
is one form not included in this number, which appears to be com-
mon to Britain and Texas, C. depressa, Salter ; and this, in Wales,
makes its appearance in the Tremadoc slates; and in America an-
other form, C. Zenkeri, Bill., is found in the Quebec group.
In the Old World eighteen species of the genus Conocoryphe occur
among the representatives of the Lingula-flags and the underlying
deposits, and four forms make their appearance in the Tremadoc
slates.
In America this genus does not range so high as the genus Olenus ;
and in the same country it has been met with in a lower horizon
than Olenus.
Of the genus Microdiscus one form is mentioned by Dr. Dawson
as occurring in the primordial rocks of New Brunswick, and one form
appears also in the Quebec group.
Wales affords two species of this genus, one of which is found in
the Menevian series, and the other in the purple rocks of St.
Dayid’s. This genus also ranges higher in America than in the
Old World.
As regards Arionellus, four species have been recognized in the
Potsdam sandstone of America, and two have been obtained from
the Quebec group. In Britain, and on the continent of Europe,
three forms occur; and these are found low down among the earlier
rocks.
This genus also appears in a higher horizon in America than in
the eastern hemisphere.
Of the genus Dikelocephalus there are in the Potsdam sandstone
of America twelve forms; and in the Quebec group thirteen species
occur. In Britain, which seems to be the only country where this
genus occurs in the Old World, there are four forms ; and these have
a limited range, three being confined to the Upper Lingula-flags, and
one to the Tremadoc slates.
Here, again, we have a genus which is represented in a higher po-
sition in America than in Britain.
[May 10,
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
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HARKNESS AND HICKS—ST. DAVID’S PROMONTORY. 397
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398 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
The genus Paradowides is represented in America by six species ;
and these all appear to occur in the lower portion of the primordial
zone. Of these species it seems probable that P. Z’hompsoni and P.
vermontianus, which Mr. Billings has referred to a new genus, Ole-
nellus, occur in a position higher than the forms from Massachusetts ;
and as regards P. macrocephalus, Emmons, its position seems to be
doubtful *. The Old World affords, including the new species alluded
to in this communication as occurring in the purple and green rocks
of St. David’s, twenty forms; and these are all very low down in the
earliest fossil-bearing rocks of Britain. and Europe.
The genus Anopolenus, very nearly allied to Paradoaides, affords
two species only ; and these have hitherto only been found in the dark-
coloured rocks above the purple and green strata of St. David’s; and
the same remark applies also to Hrinnys and [Holocephalina, a species
of each of which occurs in the same rocks.
As regards the thickness of the strata extern to the British isles
which afford the earlier forms of Trilobites, this, in Europe, contrasts
very strongly with what our own country exhibits.
In Sweden, the strata representing the ancient fossiliferous rocks of
St. David’s are very thin, if we regard them as included in Angelin’s
“‘ Regio B.” Itis, however, by no means improbable that in this coun-
try the underlying ‘“fucoid sandstones” represent the lowest series
of the fossiliferous rocks of South Wales.
In Bohemia, the primordial zone of Barrande, “ Etage C,” has a
thickness of about 1200 feet.
The thickness of this zone in Spain seems to be very small. There
are two bands representing the primordial rocks in that country.
One has a thickness of about 40 metres, that of Sabero ; and the other
seems to have a like thickness. They may, however, be the same
band repeated by a fault.
In America the Potsdam sandstones, or their representatives, have
very variable thickness. In some spots they are not more than
20 feet in depth, while in other localities they are said to attain to
several thousand feet of thickness.
In Wales, if we assume the strata to which the term Lingula-flags
has been applied, and those which in South Wales occur in a lower
horizon, to represent the Potsdam sandstones, then we attain to a
thickness much exceeding even the most extensive development of
these sandstones, since the Lingula-flags would afford us about
6000 feet of strata where they are best developed, to which we
have to add from 3000 to 4000 feet for the St. David’s rocks in which
fossils occur, as shown by the labours of Mr. Hicks.
Last of Memoirs published since 1862 on the Rocks of the St. David's
Promontory, and on their representatives in North Wales.
1. Salter, Quart. Journ. Geological Society, Feb. 1863.
2, Hicks, Trans. of the Geol. Soc. of Liverpool, Dec. 1863.
3. Salter, Quart. Journ. Geol. Soc. 1864.
* The form P. asaphoides, Emmons, seems to be an Olenus.
1871.] HICKS—TOSSILS FROM ST. DAVID’S PROMONTORY. 399
4, Salter & Hicks, Report Brit. Assoc. 1865.
5. Salter & Hicks, Quart. Journ. Geol. Soc. 1865.
6. Plant, Quart. Journ. Geol. Soc., and Trans. Geol. Soc. Man-
chester, 1866.
7. Salter & Hicks, Report Brit. Assoc. 1866.
8. Salter & Hicks, Quart. Journ. Geol. Soc. 1867.
9. T. Belt, Geol. Magazine, 1867.
10. Davidson, Geol. Magazine, 1868.
11. Hicks, Report Brit. Assoc. 1868.
12. Salter & Hicks, Quart. Journ. Geol. Soc. 1869.
Descriprions of New Species of Fossizs from the Lonemynp Rocks
of St. Davin’s. By Henny Hicks, Esq.
Proutonta Sepewicki1, Hicks. Pl. XY. figs. 1-8.
A large Trilobite having affinities with Paradowides and Anopo-
lenus in the form of its glabella, but differing from them in having
the whole of its surface covered with coarse tubercles or spines.
No perfect specimens have been found, but numerous fragments,
including glabella, cheeks, head-spines, and portions of the thorax.
These, however, show a form nearly equal to Parad. Davidis in size ;
and it is therefore, next to that species, the largest Trilobite discovered
in British Cambrian rocks. The head is semicircular, with a wide
margin and tolerably long posterior spines. The glabella is large,
strongly convex, wider than the cheeks, and reaches ‘anteriorly to
the frontal margin; it has three complete transverse lobes, and one
incomplete lobe on either side, and is widest across the anterior
lobe. Cheeks triangular. Eyes large, extending from near the
anterior furrows of the glabella to about half of the length of the
cheeks. The thoracic segments show also a strongly tubercular
surface. The axis is wide and slightly convex. Pleure long and
deeply grooved, and with the spines bent backwards.
Locality.— Headland near Nun’s well, St. David's.
ParapoxipEs Harxyessi, Hicks. Pl. XV. figs. 9-11.
Of this species the head and some fragments only have been found ;
but these show a species entirely distinct from any previously
discovered in Britain, although resembling the Bohemian species P.
rugulosus. ‘The eyes reach the whole length of the cheeks, and are
strongly raised at each extremity. The glabella is large, reaches
far forwards, and is indented by three complete furrows, and two
incomplete ones on either side.
Locality.—Headland near Nun’s Well, St. David’s, and on road-
side between Solva and Whitchurch.
Conocoryrue Lyrtui, Hicks. Pl. XVI. figs. 1-7.
An exceedingly well-defined species, and the earliest known of
the genus. It occurs tolerably plentifully, and in a well-preserved
state. Ovate in form, surface generally raised, and more or less
convex. Length from 14 to 2 inches, breadth from 1 to 13 inch.
400 PROCEEDINGS OF THR GEOLOGICAL SOCTHTY. [May 10,
Head strongly marginate, semicircular, and with a smooth sur-
face; angles produced into short spines, directed backwards. Gla-
bella parabolic and convex, and indented by three very distinct
lateral furrows which reach about one-third of the distance across.
Cheeks wider than the glabella, and raised. Eyes situated at
about one-third of the distance across from the glabella, and con-
nected with the glabella by very strongly marked ocular ridges.
The facial sutures run outwards and forwards above the eyes,
and backwards below the eyes to the posterior margin, a little to
the inner side of the spinous angles. Thorax consisting of four-
teen segments ; the axis is convex and tapers gradually towards the
tail. Pleure less than half as long again as the rings of the axis,
grooved deeply, and bent backwards from the fulcrum, which is
situated about midway. Tailsemicircular, with a tapering, strongly
raised axis of four segments; limb marked with four distinct ribs.
This species approaches nearer to CO. applanata than to any other
Cambrian species, but is of larger size, has the eyes placed much
nearer the glabella, has shorter pleurz, and a more strongly ribbed
tail.
Locality.—A headland near Nun’s Well, St. David’s.
ConocoryPHE sotvensis, Hicks. Pl. XVI. fig. 8.
The head and a few thoracic segments only have been found; but
these are sufficient to mark a new species, resembling in some respects
the Bohemian species C. coronata. The head is semicircular, tuber-
cular all over, and strongly marginate. Glabella small, reaching
less than two thirds of the distance forwards, narrow anteriorly, and
indented by three lateral furrows. A strongly raised boss occupies
the place anterior to the glabella, and reaches from it to the margin,
but is separated at the base from the glabella by a deep furrow.
Cheeks more strongly convex than the glabella, and about twice
as wide; the cheeks are wider than in C. coronata; and it seems
altogether a wider form.
Locality.—Road-side between Solva and Whitchurch, St. David’s.
Micropiscus scutetus, Hicks. Pl. XVI. figs. 9 and 10.
Differs from Microdiscus punctatus, the only other species found
in Britain, by having the lobes of the tail distinctly ribbed and not
punctated ; is about equal to it in size.
Locality.— Headland near Nun’s Well, St. David’s.
AGNOSTUS CAMBRENSIS, Hicks. Pl. XVI. figs. 11 and 12.
About one fourth of an inch long, and convex. Head longer than
wide, and straight on the sides. Glabella occupying more than a third
of the width, and divided at its anterior third by a transverse
furrow. Tail nearly of the same shape as the head, with a wide
axis centrally raised and indented by three furrows on each side.
Locality.x—Headland near Nun’s Well, St. David’s.
Tueca antrqua, Hicks. Pl. XVI. fig. 13.
About # of an inch long; surface not corrugated, and extremity
1871.] HICKS—FOSSILS FROM ST. DAVID’S PROMONTORY. 401
rather blunt. Differs from Theca penultima and Theca corrugata in
having a smooth surface, and from Theca stiletto in being a larger
and wider form, and with a blunt extremity.
LinevLetia primmya, Hicks. Pl. XV. figs. 13, 14.
Half an inch in length and about 2 of an inch in width. Some
of the valves show a tolerably convex form, and are marked with
concentric lines of growth; most, however, are much compressed
and drawn out of form by the cleavage which has affected the beds
in which they occur. It is altogether a much larger species than
Lingulella ferruginea, which also is found in the same beds. It is
moderately plentiful in the red beds at the base of the purple sand-
stones at Caerfai, Nun’s Well, and Porth Clais harbour, on the coast
to the south of St. David’s; but as the beds in each case are much
cleaved, good specimens are seldom found.
LeperpitiA ? cAMBRENSIS, Hicks. Pl. XV. figs. 15-17.
Valves about 7 of an inch long, by about 4 of an inch in width.
Some of the specimens show a reticulated ornamentation entirely
distinct from the ordinary lines of growth ina Lingulella, which makes
it probable that they belong to the genus Leperditia. In other
respects the characters are rather indistinct ; and though specimens
are very plentiful in the red beds along with Lingulella primeva,
the cleavage has so affected them that it becomes difficult to recog-
nize their true form, or to note any special characters.
Prorosponera ? Mayor, Hicks. Pl. XVI. figs. 14-18.
The specimens figured under this name I have possibly incorrectly
referred to the genus Protospongia; but as they approach nearer in
character to that genus than to any other yet described from the
earlier rocks, I may be pardoned for doing so in preference to making
a new genus, where the nature of the fossil is so indistinct. The
specimens, however, have very definite characters, and are entirely
distinct from those markings so common in the Cambrian rocks, and
usually classed together as worm-tracks. In many cases the lines
cross each other at sharp angles; at other times a branching appear-
ance is given; nearly all appear asif two flattened fibres were joined
together longitudinally, one being wider than the other. At present
only a few associated beds, almost immediately below those con-
taining Plutonia Sedgwicku, have yielded these fossils; but in them
the markings are very plentiful, covering, indeed, almost the whole
surface of the beds. One specimen, however (fig. 18), was dis-
covered by me some time since in the “ Menevian group.” Fig. 19
represents Protospongia? flabella, Hicks, a Menevian species, but
placed here for comparison ; it certainly in some characters resembles
Protospongia? major, and is most likely connected with it generi-
cally. Fig. 20 represents P. fenestrata, Salter, also a Menevian
species, and the first described of the genus. In this species the
VOL. XXVII.—PART I. 2F
402 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
fibres do not show the longitudinal lines always present in Proto-
spongia major, nor are they flattened ; but in this specimen the fibres
are much larger than in the one floured by Mr. Salter in Quart.
Journ. Geol. Soc. vol. xx. pl. xiii.
EXPLANATION OF PLATES XV. AND XVI.
(Illustrative of Fossils from the Longmynd Rocks of St. David's.)
PLate XV.
Fig. 1. Head of Plutonia Sedgwickii, Hicks.
la. Portion of the same, magnified.
2. Head (small) of Plutonia Sedgwickit.
3. Free cheek of P. Sedgwickii.
4. The same, large sizes
5. Margin of the head of a large specimen of P. Sedgwickit.
6, 7, 8. Pleurz and part of the axis of P. Sedgwickiz.
9. Paradoxides Harknessi, Hicks, head of.
10. , labrum.
11. —— , a thoracic segment,
12. Discina pileolus? Hicks, from the red rocks at the base of the purple
sandstones.
12 a. , magnified.
13 and 14. Lingulella primeva, Hicks.
15, 16, 17. Leperditia? cambrensis, Hicks.
15 a, 16.4, 17 a. , magnified.
18. Part of the head of a Trilobite from a bed at the base of the purple rocks,
about 3000 feet below the ‘‘ Menevian group.”
Puatr XVI.
Fig. 1-4. Conocoryphe Lyeilit, Hicks.
5-7.
, narrower form.
8. solvensis, Hicks, head of.
9. Microdiscus sculptus, Hicks.
9a. , magnified.
10. .——— ——,, tail of.
10a. tail of, magnified.
11. Agnostus cambrensis, Hicks, head of.
ll a. ——~ ——, head of, magnified.
12, —— , tail of.
12a. — ; tail of, magnified.
13. Theca antiqua, Hicks.
14-17. Protospongia? major, Hicks, from the Longmynd Rocks, St. David’s.
18. , from the “ Menevian Group,” St. David’s.
19. Protospongia? jlabella, Hicks, from the “‘ Menevian Group,” St. David's.
19 a. , portion magnified. St. David’s.
20. —— fenestrata, Salter, from the “ Menevian Group,” St. David’s.
Discussion.
Mr. Hvueues bore testimony to the admirable work done by Mr.
Hicks, who had, almost unaided, worked out the geology of that
district. Allowing that many subdivisions and new specific names
had with great advantage been introduced into petrology, he de-
Quart. Journ. Ceol. Soe. VoL XXVILPLXV.
GRDeWilde del et hth Mmtern Bros anxp.
LOWER CAMBRIAN FOSSILS FROM S*DAVIDS.
i ake
Quart . Jourm.. Ceol. Soe. Vol XXVIT PLXVL
~
20.
act
/
Cee
- seem ones Nice a
po Sete
Minterm Bros imp
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‘
LOWER CAMBRIAN FOSSILS FROM S*DAVID’S.
1871.] HARKNESS AND HICKS—ST. DAVID’S PROMONTORY. 403
fended the Survey nomenclature by reference to the then received
definition of Syenite and Greenstone, terms still imperfectly understood
and applicable to the main mass of the rocks in question, though
possibly subsequent closer examination and new sections may have
rendered some modification of the boundary line desirable. He was
prepared to allow the metamorphic origin of all rocks of the classes
under consideration, but did not think there was sufficient evidence
to show that the divisional planes in the Syenite and Greenstone of St.
David's were due to original stratification ; but they might correspond
rather to the great joints of most granites. Mr. Hughes pointed
out that the conglomerate contained fragments of the hornstone and
quartz of this older series, which he considered was probably part of
an old ridge or shoal, possibly of Laurentian, but certainly of Pre-
Cambrian age, and thought that there were slight differences in the
lithological character of the beds on either side, such as might be
explained on this supposition. He agreed with Prof. Ramsay in
thinking that there was evidence of the proximity of land in early
Cambrian times, but was not prepared to refer these red rocks to
inland seas or lakes as opposed to open sea; the whole seemed rather
the deposit of an open sea encroaching during submergence. He
did not attach very much importance to the restriction of genera to
limited horizons in these older rocks of St. David’s; for, as it
was reserved for Mr. Hicks to discover these fossils after so many
other observers had examined the district, he anticipated that
further researches must certainly result in finding links which will
connect together more closely beds the stratigraphical relations
of which seem to indicate so clearly an unbroken though varying
series.
Mr. Gwyn Jurrreys had been struck by the intercalation of non-
fossiliferous beds from time to time among the fossiliferous beds
described in the paper. Beds nowin course of formation contained
also very few, if any, organisms, apparently in consequence of the
great deposits of mud brought down by rivers and redeposited in
certain parts of the sea-bed. That this was the case had been
proved by recent dredging-operations both in the Atlantic, off the
coast .of Spain, and in the Mediterranean.
Mr. Boryp Dawxus called attention to the extension of the Mol-
luscoida, Annulosa, and Mollusca, deep down in the Cambrian rocks,
and yet without any trace of their convergence. ‘The origin of life
might be as far removed from that period as was the Cambrian from
the present time. The difference in the colours of the rocks he was
inclined to refer to the different degrees of oxidation of the iron
they contained, which might supervene in a comparatively short
time.
The Rev. W. S. Symonps had, in visiting the spot, been much
struck by the rocks, at that time termed Syenite, which he believed
might be an extension of those on the Carnarvonshire peninsula,
and which he thought supported the whole series of the Cambrian
rocks, so that they might after all be the ce the same as
E2
404 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
those of Sutherlandshire and Assynt. If this were the case the
nomenclature of the Geological Survey would have to be altered,
and the rocks of Pistyl and Holyhead no longer termed. metamor-
phosed Cambrian rocks, but Laurentian.
Mr. Hicks, in reply, stated that the quartziferous breccias form-
ing the central ridge contained so many rolled pebbles, and were,
moreover, in places so distinctly bedded, that there could be no
doubt of their being sedimentary. Other beds, described as Green-
stone in the maps of the Geological Survey, were also distinctly
laminated. The non-occurrence of fossils in the more sandy beds
he attributed to their having been deposited in very shallow water.
The fossils occurred principally in fine-grained beds of a flaggy
nature.
2. On the Acz of the Nusian Sanpstone. By Raxrpn Tare, Esq.,
Assoc. Linn. Soc., F.G.S.
Mr. BaverMAN, in a recent number of the Quarterly Journal of this
Society (vol. xxv. p. 27), has discussed at some length the opinions
advanced respecting the age of the sandstone strata underlying the
Cretaceous limestones, and resting upon the granitic and schistose
rocks, in Sinai. These rocks belong to the same series of sandstones
described by Russegger as occurring in Egypt, Nubia, and Arabia
Petra, under the name of “ Nubian Sandstone.”
Though the facts that I have the honour to submit to the Society
may be stated in a few words, yet it seems desirable to recapitulate
briefly the views that have been advanced as to the period of depo-
sition of the strata in question, the better to explain away those in-
ferences which are so much at variance with my own.
In the first place, it appears, from the circumstance of the
Nubian Sandstone being overlain conformably by approximately
horizontal strata of Cretaceous age, that this formation has been re-
garded, in the absence of paleontological evidence to the contrary,
as forming part of the Mesozoic group of rocks. Thus Russegger
colours and describes it as Lower Cretaceous in his maps; and Bauer-
man, guided by the lithological similarity of its strata to the Lower
New Red Sandstone about Chester, has placed it on the horizon of
the Trias; whilst Figari Bey seems to have regarded the tripartite
arrangement and lithological features of the series as sufficient tests
by which to assign the whole to the Trias, “ taking the limestone as
representing the Muschelkalk, although the evidence for this de-
termination (other than lithological character) is not very clear”’*.
In the second place, the fossils which have been obtained from
the limestone separating the sandstone into two great masses are,
for the most part, fragmentary, in bad condition, or otherwise unde-
terminable. Hence the paleontological evidence is of a most con-
* Bauerman, loc. e7t. p. 27.
1871.] TATE—NUBIAN SANDSTONE. 405
tradictory nature ; indeed the generic names assigned to the fossils
seem to have been given in accordance with their presumed age as
determined by the lithological characters and physical conditions
presented by the containing rocks, rather than as interpretations
of zoological affinities.
Thus the Encrinites which occur in the Nasb-valley limestone are
represented by fragments of cylindrical stems, and do not admit of
generic determination. The Ammonite, the only fossil mentioned
by Figari Bey, is not named specifically ; and I have reason to doubt
the correctness of its identification, and suspect that it may have
been either a Nautilus or a Goniatite. Mr. Etheridge and Figari Bey
have referred the fossils brought under their notice to Secondary
genera, Hncrinus and Ammonites ; whilst Mr. Salter assigned the En-
crinite stems to the Carboniferous genera Rhodocrinus and Poterio-
erimus, and adds to the list the Gasteropod genera Murchisonia and
Eulima (?), which latter are Triassic as well as Carboniferous.
So that really it has hitherto been difficult to express any very
decided opinion on the age of the Nubian Sandstone, owing to the
great want of paleontological evidence. Conclusive evidence of the
Carboniferous age of the series, however, has been recently brought
to light. Captain Wilson and the Rey. F. W. Holland, of the Sinai
Ordnance Survey, have placed in my hands a block of limestone
from the Nasb-valley section (vide Bauerman, loc. cit. p. 26) in
the hope that it would yield evidence of its age, and so of the asso-
ciated sandstones.
One fossil only, in a good state of preservation, was contained in
the mass; this I at once named Orthis Michelini, a well-known
fossil of the Carboniferous Limestone; but that the specific deter-
mination might be indorsed by the greatest authority on the fossils
of the class to which it belongs, and so acceptable as indisputable
evidence, I submitted the specimen to Mr. Thomas Davidson, who
obligingly writes, that the “‘inclosed fossil is certainly Orthis Mz-
chelint, as you correctly identify it.” With this valuable index to
the age of the limestone, the obscure forms associated therewith
may be approximately assigned to the genera indicated by Mr.
Salter, who thereupon referred these beds to the Carboniferous
epoch.
Mtr. Salter * has moreover described a Lepidodendron from Sinai
as a new species, under the name of L. Mosaicum; and though
neither the locality nor the stratigraphical position of the fossil was
known to him, yet, as it is preserved in sandstone, we cannot hesi-
tate in referring it to one or the other of the arenaceous members of.
the Nubian Sandstone; andthe Rev. F. W. Holland was fortunate in
obtaining a portion of a Sigillarian stem from the Wady Mokatteb,
which, though not collected in situ, bears unmistakable evidence
of having been enclosed in the sandstone forming its cliffs. The
sandstone in this valley is overlain by Cretaceous limestone, and is
presumably referable to the Upper Sandstone of the Carboniferous
series of this region.
* Quart. Journ. Geol. Soc. vol. xxiv. p. 509.
406 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
I append a list of the organic remains from the “ Nubian Sand-
stone ” series :—
! Orthis Michelini.. . . . . Wady-Nasb Limestone.
! Streptorhynchus crenistria . is Pe}
! Spirifera (fragments oa ; ye i
* Murchisonia . . iL Ai Bs
MMMM AR Ec. Myetuheotrememien yrs 5 ss
% Rhodocrinus ..... . x ”
'x Poteriocrinus . “ ” ”
* Lepidodendron Mosaicum Wady-Nasb Sandstone.
! Sigillaria, sp. ” ”
[The sign ! prefixed to the names of the fossils indicates that the
specimens were collected by the Sinai Survey; and the sign * in-
dicates the determination of Mr. Salter. ]
In conclusion I venture to suggest that the Adigrat Sandstone in
Abyssinia, described and so named by Mr. W. T. Blanfordy, is of
the same age as the Nubian Sandstone. It appears to have escaped
the notice of that author that the Sandstone of Adigrat is similar in
character and general appearance to the Nubian Sandstone, and
that it, moreover, overhes the schistose rocks in the same manner,
and contains iron-ore and psilomelane, as in Sinai. Mr. Blanford
surmises, however, that “ both the coal-hearing beds of Chelga and
the Adigrat Sandstone may belong to a portion of the great series
associated with [Triassic] coal in India” (loc. cié. p. 175); but the
Talcheer and other coals are referred by Messrs. Blanford and Theo-
bald to a Permian age (Mem. Geol. Surv. India, vol. i.).
Norr.—My attention has been called since the reading of this
paper to Prof. Unger’s observations on the Fossil Wood from Assuan
and Um-Ombos, in the Nile valley (Quart. Journ. Geol. Soe. vol. xv.
Mise. p. 18, 1859). The wood belongs to,a coniferous tree of the
Araucarian division, and is named Dadowylon cegyptiacum; its
habitat is assumed ‘“‘to be the sandstone, which occurs extensively
in Upper Egypt and Nubia, between the granite and Cretaceous
beds,” in which case Dadoaxylon egyptiacum was contemporaneous
with Lepidodendron mosaicum and Sigillaria. Prof. Unger argues,
from the presence of this genus, that the sandstone, ‘hitherto of
doubtful rank in the geological series, as no organic remains have
been found in it,” should be ranked in the Permian, rather than in
the Keuper or the Cretaceous formation; but from the paleonto-
logical evidence alone he might have argued equally in favour of
its Carboniferous age.
3. On the Discovery of the GLurron (GuLO Luscus) in Brrrarn.
By W. Boyp Dawkins, Esq., M.A., F.R.S., F.G.S.
THE caves in the Mountain Limestone which forms the magnificent
gorge of the Elwy, near Cefn, St. Asaph, have furnished from time
t Geology and Zool. of Abyssinia, p. 170.
1871.] DAWKINS—GULO LUSCUS IN BRITAIN. 407
to time a remarkably complete series of pleistocene mammals. That
which opens on the terraced side of the cliff in the grounds of Cefn,
first described by the Rey. E. Stanley in 1833, and subsequently by
Dr. Falconer, contained abundance of Reindeer, associated with
Cave-lion, Cave-bear, Grizzly Bear, Hyena, Hlephas antiquus, Hip-
popotamus major, Rhinoceros tichorhinus, and R. hemitechus. And
nearly all these animals occurred in a second cave, at Cefn, explored
by Mr. Williams Wynn in 1869-70. A third cave, at Galtfaenan,
explored last winter by Mr. Mainwaring and Mr. Hughes, has fur-
nished the remains of Reindeer and Bear, and the traces of Hyzenas ;
while a fourth, at Plas Heaton, in part dug out by Mr. Hughes and
Mr. Heaton, has yielded Wolf, Bison, Reindeer, Horse, and Cave-
bear, and a remarkably fine lower jaw which proves that the Glutton
inhabited Great Britain during the pleistocene, or quaternary age.
Mr. Ayshford Sanford and myself had, indeed, obtained, in 1865,
the crowns of three canines from the caves of Banwell, and Bleadon,
and of Gower, which belonged to this animal ; and we accordingly in-
serted it, without figure or description, in the list of the British
Pleistocene Mammals, published by the Paleontographical Society
in 1866. ‘This discovery at Plas Heaton renders any doubt as to its
being a true pleistocene British species altogether impossible.
The jaw consists of the left ramus, docked of the angular and
articular portions, which are broken off close behind the first true
molar. On comparison with the lower jaws of the Glutton in the
British Museum, from Norway, and also from the caves of Gai-
lenreuth and Sundwig, I find that the Welsh specimen is slightly
larger than the latter, and considerably larger than those of the
animal now living in Europe. With this exception, there is not the
slightest difference between them. The peculiar ridging and grooving
of the inner side of the alveolar border, which at first sight appears
as the accidental result of the inflammation of the periosteum, is
common to all which I have examined ; and, taken in combination
with the great alveolar width, affords a means of determining at once
a fragment of the jaw from that of any otheranimal. The premolar
and molar series, also, are crowded together in a very short alveolar
space, and occupy the upper and outer margin of the jaw, instead of
occupying its superior surface, as in the majority of the carnivores.
The peculiar wrinkled pattern of the enamel separates the teeth at
once from those of any carnivore which are likely to be confounded
with them, except the Hyzna, which is put out of court by the
larger size and different form of all its teeth except the upper incisor
3, and the first upper premolar. The first of these bears a strong
superficial resemblance to the canine of the Glutton, but is differen-
tiated by the enamel surface of the latter being more deeply and
irregularly grooved, and by the cingulum passing from the posterior to
the anterior ridge being much less prominently developed. The
upper premolar 1 of Hyzena can be determined at once from the
second lower premolar of the Glutton, which it closely resembles in its
single fang and procumbent form, by the crown of the latter being set
408 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10.
on the fang much more obliquely, and by the obtusely pointed apex
rising abruptly from the anterior border instead of sweeping nearly
equally upwards from the posterior and anterior borders. The pre-
molar series of the Glutton may be separated from that of the Canidee
and Felide by the great transverse thickness of its teeth, and the ab-
sence of the anterior and posterior accessory cusps. The first lower
true molar is distinguished at once from that of the Canide by the
stoutness and obtuseness of the two sectorial blades, and by the
non-development of a cusp on the postero-inner edge of the base
of the posterior blade. The tubercular portion also of the Glutton
is much smaller and more talon-like (consisting of a very obtuse
triangular cusp) than in any of the Canide. With these excep-
tions, I do not know of the teeth of any carnivore with which those
of the Glutton under consideration can be confounded.
The following Table shows the relation of the lower jaw of the
Glutton from Plas Heaton to those found in the caves of Germany,
and to a recent specimen preserved in the British Museum. The
Welsh fossil in every dimension is larger than any of the rest, and
must have belonged to an animal proportionally more robust than
any of the others. The measurements are taken in decimals of an
inch.
B i
S diliee g 2 4
Sh (Becl.ne0al 980 deer
sa a) ae E eb
2 = zc) s ‘S
Fs locos chalet tat Wee een ee!
Ay ) RM M il
Alveolar space occupied by molar series
from Pry Ovo nVieg arches ee eeeenene 1°95 | 1°9 1:85, | WSO. ce7e
Depth of ramus beneath Pm. 2.......... Vl 0795 | 0°98 | 07995 | O9
Depth of ramus beneath M. 1............ 0°96 | 08 o796 | 0795 | 0°85
Length of crown of canine ............... o°8 0°82
Antero-posterior measurement] c'29 | 0°24 | c'24 | 0°28 | 0°25
Pm. 2.4 Transverse 59 o'2 or1g | O18 | O18 | O15
Vals velba orperenaassneacosetsceouss o'2 Ori || CrPuG || Geng Ih eng
f Antero-posterior measurement} 0°36 | 0°36 | 0°35 | 0°35 | 0°34
Pm. 3. ] Transverse 3 0124 | 0°23 | O21 | o2 o2
Height...... GODENB SBagoao SEs RCOSTON 0°24 | 0°23 | o'21 | O22 | O2
Antero-posterior measurement] 0°5 O75 0°5 045 | 049
Pm. 4. Transverse - O73), | JO:20 |) 60 Oo ls miaaay
JaIGTA MERE ob isadandsaSheanaeoesonde: 03 029 | 0129 | c'28 | 026 |
Antero-posterior measurement} o'95 | 0°92 | 0°88 | cg 0°82 |
M. 1. 4; Transverse i 0742 | O74 0°38 | 04 0°34.
aly ed itipioponossnctecdbecnadannnocare 042 | 04 on O74 036+
I am able to detect no specific difference between the G'ulo speleus
of Goldfuss, from Germany, and the living form, G'ulo luscus of Lin-
neus. The fossil carnivore was larger than the living, probably
because in pleistocene times the competition for life was not so keen
as it is now among the mammalia. Man in those early times had
1871.] DAWKINS—GULO LUSCUS IN BRITAIN. 409
not increased and multiplied to such a degree as to upset the ceconomy
of nature, by driving the wild animals away from their feeding-
grounds, and robbing the carnivores of a large portion of their food.
To this cause I should assign the larger size of nearly all the pleis-
tocene mammalia, as compared with those which are undoubtedly
their lineal descendants, such as the Cave-lion, the Cave-hyzna,
and the Stag.
The Glutton at the present day inhabits the inclement northern
regions of the Old World, to the point where the forests gradually
die down into the lonely wastes of the “‘ Tundras,” and is to be
found in Norway, Sweden, Lapland and as far east as Kamtschatka.
In the New World it ranges, under the name of Wolverine, north-
wards from the latitude of Canada. It was seen by Ross in the 70°
parallel in the winter; and its bones have been met with in Melville
Isiand. Its southern limit in Asia is the latitude 50°, where it
occurs in the Altai. In Europe its southern limit is not clearly de-
fined; but it has steadily retreated northwards as the vast forests of
Germany and Poland gradually fell under the axe of the woodman.
According to Eichwald, it once lived in the Lithuanian region along
with the Bison, which still lingers there under the protection of an
Imperial ukase ; and Zimmermann adduces proof of its having been
. killed as far south as Helmstadt, in Brunswick*. In the pleistocene
caves of Germany it is found abundantly, with the Reindeer, Cave-lion,
and Hyzena, at least as far south as Gailenreuth, in Bavaria, where
it was first discovered by Dr. Goldfuss. It is figured and described
from the caves of Belgium by Dr. Buckland’s great rival, Dr. Schmer-
ling. We might therefore naturally expect to find the animal
ranging over our island at a time when it formed part of the main-
land of Europe, and offered free access to the same animals (the
Reindeer, the Lemming, and the Horse) as those which still furnish
food to the living Glutton in Siberia. The presence in Great Britain
of a creature adapted for enduring the severity of an Arctic winter,
and not now found in any hot regions, along with the Rein-deer,
Lemming, and Musk-Sheep, implies that the pleistocene winters were
of an Arctic severity—just as the Hippopotamus, found under precisely
the same conditions, and associated with the same group of animals,
points to a hot summer like that which obtains on the Lower Volga.
The intimate association in one spot of animals now confined re-
spectively to the hottest and coldest regions seems to me to admit
of no other explanation.
IT have added to this essay a list (see p. 410) of the pleistocene
animals found in the various caves hitherto explored in the valley
of the Elwy, as supplementing the Table of the Distribution of
the British mammals published in the Quarterly Journal, May
1869.
* The authorities consulted for the range of the Glutton are Blasius (Fauna
der Wirbelthiere Deutschlands), Zimmermann (Specimen Zoologiz Geographice),
and Sir John Richardson (Fauna Boreali-Americana).
410 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 10,
a cee
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Waratisispelseusi accuse cece ej eeereecee * x @ *
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Choi WETS “pacgobodsoecacdsocadoceo ousncss oe *
Mielesita xis) ee cceercesscesseaenlelslcsesesi x Bu 200 *
(Opnanis) WUUOSS: dadcencconaspansasabooossouHa6du * * A66 *
= INN NWIE, cacccneadscoda0sco0 0000900000000 * * ie *
Hyena spelzea .........scsseee.sssseereerss * * * x
Cervus tarandus ............s..0s.seeseeeee # x # *
ClapbUs\tessona set oteeset en cdtaseecstac t x
BiSOM PLISCUS......2...0. ..0esecccerernrnsee * *
Hippopotamus major ............s00....5- * *
Equus caballus ..........0......-sseceeeeeee * *
Rhinoceros hemitcechus .0.......,00-....] ¥ *
(HOLVOTARIAIEIS Gon Goncbecnqobasoqaddbe080e *
Hlephas antiquus .....+........,sececeeeeess * %
Arvicola amphibia ..................02005- x
From this list all reference to the series of prehistoric mammalia,
and to the traces of prehistoric man, has been omitted.
Discussion.
Mr. Hveuss indicated the exact position in which the jaw of the
Glutton was found, but pointed out that, owing to the excavations of
keepers, Badgers, Rabbits, &c., the earth was so much disturbed in
that part that it was impossible to be sure of the original relative
position of the bones. He showed that the Plas Heaton Cave was
on a hill rising from the top of the plateau, while the Cefn, Brysgill,
and Galtfaenan Caves were in the gorge cut through that plateau,
and therefore that the Plas Heaton Cave was probably formed, and
might possibly have been first occupied, at a much earlier period than
the others. As it appeared to pass under that part of the hill which
is overlapped by heavy drift, he thought it quite possible that this
may have been a preglacial cave, and that by-and-by we may find
evidence of a preglacial fauna in it.
The Rev. W. 8. Symonps mentioned that in some of the pot-holes
in the roof of the Cefn cave he had procured silt containing remains
of shells determined by Mr. Jeffreys to be marine.
Mr. Hveues explained that these shells had probably been washed
in from the superficial marine drift of the district.
Mr. Dawxins, in reply, expressed his belief that though the ex-
cavation of the caves in question might have taken place at different
periods, yet that their occupation was, geologically speaking, con-
temporaneous.
~
1871.] LOBLEY—BRITISH LAMELLIBRANCHIATA. 411
May 24, 1871.
George Mosley, Esq., 7 St. Paul’s Square, York; Alexander Col-
vin, Esq., B.A., of Barham Lodge, Weybridge; Thomas Shepherd
Noble, Esq., F.R.A.S., Lendal, York; and Edward Charles Davey,
Esq., of Wantage, were elected Fellows of the Society.
The following communications were read :—
1. On the Principat Features of the StratieRaPHIcAL DistRiBv-
TIon of the British Foss Lamenniprancniata. By J. Logan
Losey, Esq., F.G.S.
Havine been engaged for some years past in investigating the
organic contents of British strata, and in the enumeration of the
species which have been recorded as occurring in each geological
formation, I am enabled to bring before this Society a summary of
the stratigraphical distribution of the remains of one of the classes
of the Mollusca, the Lamellibranchiata, as far as it is at present
known. *
The results here presented are submitted with confidence in their
reliability as being approximately correct to the present time, since
well authenticated species only have been retained in my lists, and
extreme care has been taken to exclude those numerous synonyms
which are so frequently productive of incorrect conclusions.
The class Lamellibranchiata cf De Blainville, or Conchifera of
Lamarck, is represented in British strata so abundantly that the
genera alone number nearly two hundred. I will not here attempt
to give the details of the range and distribution of these very nume-
rous genera, but confine myself at the present time to the consi-
deration of the principal groups of the class.
The classification of the Lamellibranchiata that will be followed
is founded on that of Lamarck, and differs little from the one given
in the excellent and much used Woodward’s ‘ Manual of the Mol-
lusea.’
In the accompanying Tables the usual geological scale has been
adopted. The term Silurian is intended to embrace all the rocks
included by Murchison in this “System,” namely, from the Lingula
Flags to the Passage Beds. Triassic includes the Rheetic Beds, and
Jurassic the Lias and the Oolites.
Table I. (opposite) is intended to show the stratigraphical range
as well as the increment, decrement, maximum development, and
relative numerical importance of the representation, in our area,
of each of the families of the Lamellibranchiata, remains of which
occur in the fossiliferous rocks of the British Islands.
In this Table an asterisk standing alone indicates the occurrence
of a number of species not exceeding ten, two asterisks indicate the
occurrence of more than ten and less than twenty species, three
asterisks more than twenty and less than thirty, and so on, each
asterisk after the first representing ten species. The number of
Taste I.
To face p. 411.}
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412 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
species is also indicated by numerals ; but it is not intended that these
numbers are to be regarded as other than a record of what has been
already arrived at by paleontological investigation. Further re-
search will add much to our knowledge not only of the forms con-
tained in each series of strata, called by the not altogether satisfac-
tory name formation, but also of the generic and family affinities
of the species at present recorded.
The names of the families are arranged in the order of their in-
coming or earliest appearance in British strata. We can thus see
at once the relative antiquity of the various families, so far as it is
indicated by the results of research confined to the British area.
From this Table it will be seen that all the genera represented in
our rocks may be classed under twenty-two heads, or patronymic
designations. As no species of the family Tridacnide has yet been
discovered in British strata, that name does not appear in the table.
Though not occurring in the strata of these islands, species of
Tridacna are found in the Miocene deposits of Poland.
The first family mentioned in Table I., the Arcade, ranges from the
Llandeilo rocks to the most recent, and has species living in our pre-
sent seas. The maximum development of the Arcade was in the
Jurassic epoch, though the species from any one formation of that
system of rocks are not equal in number to those from the Carboni-
ferous Limestone. A large number of species of Arcade, chiefly of
the typical genus Arca, have been taken from the Cretaceous strata,
and a still larger number (upwards of seventy) from Tertiary deposits.
The Cardiide and Astartide also commence in the Llandeilo rocks,
and have equal ranges with the Arcade, though not a similar distribu-
tion. The former of the two families, Cardiude, did not attain its
greatest development until the Older Pliocene or Crag period, while
the Inferior Oolite has hitherto yielded the largest number of species of
Astartide, though the specific forms of this family are almost equally
numerous in the Older Pliocene deposits. But though the maximum
number of species of Astartude have been obtained from a Tertiary
formation, the Jurassic system gives us a much greater number of
species than all the Tertiary formations. With the exception of the
Carboniferous Limestone, the Palzozoic rocks have furnished us
with few species of either Astartide or Cardiade.
Four families, the Mytilide, Aviculide, Cyprimde, and Trigomade,
commence their ranges in Caradoc strata ; and two of the four (Mytz-
lide and Aviculidew) are represented by a considerable number of
species in those rocks. In the Devonian system the Mytihde are
sparingly represented ; but when we rise to the Carboniferous Lime-
stone we find this family largely developed. The Jurassic rocks,
however, yield the greatest number of species of Mytilidw, upwards
of seventy having been described from the Jurassic strata of Britain.
A much smaller number have been found in Cretaceous and Tertiary
deposits, though the typical genus of the family, Mytilus, is abun-
dant at the present day in the form of the common mussel (Mytilus
edulis).
The distribution of the Aviculid@ is very extraordinary, since we
1871. | LOBLEY—BRITISH LAMELLIBRANCHIATA. 413
find in one formation, the Carboniferous Limestone, a singularly great
development of one of the genera of the family, the Aviculopecten of
M‘Coy. The number of species of Aviculopecten taken from these
rocks amounts to upwards of eighty. These with the species of the
other genera of the Aviculide found in the Carboniferous Limestone
make up a total of about 150 species of this family which have been
furnished by the Mountain or Carboniferous Limestone of the Bri-
tish Islands. Compared with the enormous development of the
Aviculide in Carboniferous strata, the family is very moderately
represented in Jurassic and Cretaceous rocks, while Cainozoic depo-
sits have yielded not more than one or two species. Indeed the
representation of the Aviculide is as remarkably small in the Ter-
tiaries as it is remarkably great in the Carboniferous rocks.
The Cyprinide, though ranging from Lower Silurian rocks, are not
represented by a large number of species in any formation; and the
family attains its maximum development in the Jurassic system.
Though the typical genus of the 7rigoniade is characteristic of
Mesozoic strata, yet we have a genus, Lyrodesma (represented, how-
ever, by only one species, and placed by Bronn amongst the Arcade),
carrying the range of this family down to the Caradoc rocks. The
greatest number of species of Tvigoniade have been furnished by
the Inferior Oolite; and these are all of one genus, and that the
typical one of the family, Trigonia. Although the genus Trigonia
has not been found in any other rocks than those of Mesozoic age,
yet living Trigonie inhabit the waters on the coasts of Australia.
One or two species of the family Anatinide have been found in
Silurian rocks, and not more in Devonian strata; but the Car-
boniferous Limestone has given us upwards of forty species. By
far the greatest number of species, however, have been taken from
Jurassic rocks, which have yielded upwards of one hundred and
thirty species of this family. A great decrement is found in the
Cretaceous system, which gives us about an equal number of species
of Anatinide with the Tertiary deposits.
The Tellinide are very few in the Paleozoic and Mesozoic rocks,
and attain their maximum development in Middle Eocene strata, in
which the specific forms of the typical genus Tellina are very nu-
merous.
The estuarine and fluviatile Unionidae, as might be expected, are
not numerous in the stratified rocks of Britain, which are chiefly of
marine origin. The estuarine Wealden deposits furnish us with
the greatest number; and the fluviatile beds of the Newer Pliocene
yield several species of Unionide.
The Myade commence with a species of Corbula in the Middle
Devonian, and have but a moderate number of species in any forma-
tion. They attain their greatest development, both of generic and
specific forms, in the Tertiary strata.
Of Solenide, the species in any rocks older than those of Tertiary
age are very rare. These later deposits, however, have given us
upwards of twenty species of this family.
No fewer than six families, the Veneride, Pectinide, Lucinide, Os-
[May 24,
CEEDINGS OF THE GEOLOGICAL SOCIETY.
PRO
414
Taste II.
; 12
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*sn0s0¥q019 | FOES CEEOL x | FEI IHR E:
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Orders or Sections.
ASIPHONIDA
SIPHONIDA
LOBLEY—BRITISH LAMELLIBRANCHIATA. 415
1871.
Taste III.
Q
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Class.
LAMELLIBRANCHIATA
416 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
treide, Mactride, and Pholadide, commence their ranges in the
Carboniferous Limestone. Of these six families, four (Veneride,
Lucinide, Mactride, and Pholadide) attain their maximum deve-
lopment in the Tertiaries, and two (Pectinidw and Ostreide) in
Jurassic strata.
The small family Gastrochenide, of which but few species have
been found in British strata, has its earliest representative in the
Lias, and its greatest number of species in Tertiary strata.
The fluviatile Cyrenide also range from the Lias, and, like the
Gastrochenide, have their maximum development in the Tertiaries.
The remaining two families, Chamide and Hippuritide, are nu-
merically unimportant, and yet are structurally perhaps the most
remarkable of all the Lamellibranchs, some of the forms of Chamidee
strongly resembling Gasteropods, and the Hippuritide being so ab-
normal in form and structure as to have been for a long time con-
sidered a separate order, the Rudistes of Lamarck. The Hippuritide
are also of great interest, as being the only extinct family of the
Lamellibranchiata as yet discovered. They are represented in the
British Islands by only one species, the Hippurites, or Radvolites
Mortoni of Mantell; and this species is confined to the Upper Green-
sand and Chalk.
Though we are able somewhat satisfactorily to divide the Lamel-
libranchiata into families, there are not sufficiently good distinctions
for ordinal divisions. The fact of some genera, however, having
only one adductor muscle has been seized as a basis on which a
division of the class into the orders, groups, or sections Monomyaria
and Dimyaria has been made. This division, though perhaps not a
sufficiently scientific or philosophical one, is in some respects con-
venient, and it has been adopted by several authors.
A better division of the Lamellibranchiata than into Monomyaria
and Dimyaria is perhaps that founded on the possession, by a large
number of genera, of respiratory siphons, and some being unpro-
vided with those organs. ‘This great structural difference naturally
divides the class into Asiphonida and Siphonida—the Siphonida, or
those furnished with respiratory siphons, including by far the greater
number of genera. These two great sections of the class have an
equally extended range ; but the As¢phonida have their greatest de-
velopment in Jurassic rocks, while the greatest number of species of
Siphonida have been furnished by Tertiary strata. It may be men-
tioned, however, with respect to the former section, that although
the Jurassic system, which includes all beds from the Lower Lias to
the Purbeck, yields a greater number of species of Asiphonida than
any other of the great groups or systems of rocks, yet when we
compare formations we find that no single formation equals the Car-
boniferous Limestone in its yield of species of this division of the
Lamellibranchiata. (See Table IT.)
The distribution of the entire class now demands our attention ;
and disregarding generic, family, ordinal, or sectional divisions, and
having regard only to species, we find the Lamellibranchiata spa-
ringly represented in the lower division of the Lower Silurian group ;
1871. | LOBLEY—BRITISH LAMELLIBRANCHIATA, 417
but when we ascend to the upper division and to the Upper Silurian
rocks, Lamellibranchs are numerous. In the Devonian system a
much smaller number of species than is yielded by Silurian rocks
rewards our search. The Carboniferous formations, however, give
us a greatly increased number, nearly four hundred species having
been described as occurring in these rocks. The numbers of Per-
mian and Triassic species are small; but Jurassic strata have
furnished us with upwards of a thousand species of Lamellibran-
chiata, the Jurassic epoch having witnessed the maximum develop-
ment of the class. The number falls to about half in the Cretaceous
system, and rises again in the Tertiary deposits, strata of the latter
age having furnished to science between six and seven hundred spe-
cies of fossil Lamellibranchs. (See Table III.)
We thus see that the Lamellibranchiata have had a great develop-
ment in each of the three great epochs of geological time, the
Paleozoic, the Mesozoic, and the Caimozoic, and have undergone great
modifications of form during the long period required for the depo-
sition of the sedimentary portion of the crust of our globe. As in
other classes of the animal kingdom, some genera have lived on
through many of the great cosmical changes which our planet has
seen, while other generic forms have existed during only a compa-
ratively brief portion of the earth’s history.
Many and grave questions are suggested by this fact, a fact well
known to students of science, but the elucidation and explanation
of which are at the present time sought for by our most earnest
thinkers, and form the battle-ground, so to speak, for the contests
of the ablest and most richly furnished intellects of our day and
generation.
Discussion.
Mr. Eruerince, after noticing the importance of the paper, re-
marked that possibly the great difference observed in the propor-
tions of the Lamellibranchiata in different formations might to some
extent be due to our want of knowledge. Of late years, in the
Caradoc and Lower Silurian series, the number of species had been
nearly doubled, principally through the persevering industry of one
single observer, Lieut. Edgell. The same was to some extent the
case with the Carboniferous rocks, owing to the collections of Mr. Car-
rington. Much was also being done for the Oolitic series, in con-
nexion with which the names of Mr. C. Moore, Mr. Sharp, and
Dr. Bowerbank cought to be mentioned. Mr. Griffiths and the
Rev. Mr. Wiltshire were doing the same work for the Gault. What
the late Dr. 8S. P. Woodward had done as to the distribution of the
different species of mollusks through time, Mr. Lobley was doing on
a larger and more extended scale.
Prof. Ramsay was glad to find that Mr. Lobley was, to some ex-
tent, doing the same for the Lamellibranchiata that Mr. Davidson had
done for the Brachiopoda. He did not know how the case might
be with the Silurian and Devonian formations ; but in the Carboni-
VOL, XXVII.—PART I. 26
418 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
ferous strata the Lamellibranchiata were obtaining a preponderance
over the Brachiopoda. He accounted for their comparative absence
in formations of other ages, especially between the Upper Silurian
and Rheetic beds, by the best-known areas of those periods having
been mainly continental, or containing principally freshwater or
inland-sea remains, so that the true marine fauna was absent. In
Carboniferous times possibly the true relative proportions of the
two forms had been preserved in the deposits.
Mr. Jupp was doubtful as to the safety of placing too great reli-
ance upon figures.. He questioned whether some of the conclusions
as to the great increase of Lamellibranchiata between the Carbo-
niferous and Jurassic periods could be substantiated. Much de-
pended on the amount of the rocks present in different countries,
and the study bestowed on each. The conditions also for the pre-
servation of the fossils might be more favourable at one time than
another.
Mr. Carruruers considered the tables of the greatest value, as
indicating the present state of our knowledge. He called attention
to the difference of conditions under which different deposits had
accumulated, which must have to some extent affected the propor-
tion of Lamellibranchiata preserved in the different formations.
Mr. Cuartesworrn remarked on the occurrence of Trigonia in the
Australian seas, and on there being varieties of form among spe-
cimens of existing species so great that if they were found fossil
they might be regarded as of several species.
Mr. Hueues considered that the data were too incomplete to
justify the generalizations of some of the previous speakers. It had
been pointed out that whenever the Tables showed a very large
number of Lamellibranchs from any formation, that formation had
been carefully worked out by local observers; and therefore he
should like to know in each case the proportion the Lamellibran-
chiata bore to the total number of fossils found. It had been shown
also that a larger proportion of Brachiopoda had been found in the
older rocks, and of Lamellibranchiata in the newer. But in the
older rocks whole genera of Lamellibranchs are confined to horizons
and localities which are not cut off by stratigraphical breaks, such
as would allow us to think it at all probable that they can be cha-
racterized by peculiar genera. He thought the scarceness and irre-
gular occurrence of Lamellibranchs in the older rocks could be best
explained on the supposition that those portions of the older deposits
which were least favourable to Lamellibranchs happened to be those
now chiefly exposed to our search, and that those few portions are
only in part worked out.
Mr. Juyxins observed that in thick deposits there was a far
greater likelihood of numerous forms being present than in thin:
for thickness meant time, and time meant variation.
Prof. Morris dissented from this view, as in thin littoral deposits
an enormous number of shells might be present, while in beds formed
in deep sea they might be almost entirely absent.
1871. | SAWKINS—-BRITISH GUIANA. 419
2, GroLoercas, OpseRvAtTions on Britisa Gurana.
By Jamus G. Sawxrns, Esq., F.G.S.
A DETAILED geological survey of British Guiana, in the present state of
the colony, would be a very difficult and prolonged undertaking, as the
only lands not covered by dense forests are the coast alluvium, and
the savannas or prairies of the interior; few roads extend beyond
the sugar plantations on the former, and few Indian tracks over the
latter; therefore it must be understood that my observations were
chiefly confined to the rivers.
Along the coast the land is low, at many places (as at Georgetown)
below the sea-level, composed entirely of sands, clays, and marine
débris brought down by the larger rivers, which have been fre-
quently silted up into lakes by the contra-action of the waves of the
Atlantic ocean. The extent of this alluvium varies from ten to forty
miles inland, where it terminates in low sand-hills of 10—70 feet
elevation above the sea-level. These sand-hills extend inland until
they are seen resting on granite. They are somewhat rounded by
the action of the water of insignificant streams and rain.
The amount of rain, according to observations by Mr. Sandeman
during ten years, shows an annual average of 102-826 in., the
minimum being 68-680, and maximum 133-219; these facts will
convey an idea of what the denuding influences in this colony are.
My first excursion was limited to what is called the Pomeroon
district, comprising the Waini, Barama, Barima, and Pomeroon
rivers. The first granite was observed on the Wainii and Canyaballi,
just below the mouth of the Barama, where it is much weathered
and worn into deep furrows, particularly under the rain-droppings of
large trees; the crystals of quartz, withstanding the effects of exposure
longer than either the felspar or mica, protrude on the surface
very remarkably.
To the south-west of the junction of the Wainii and Barama there
is a depression covered with alluvium or with lakes, ponds or bayous ;
then rise granite, gneiss, and mica-schist, often friable on the surface
from the decomposition of iron pyrites ; dykes of greenstone traverse
the schistose rocks, and indurate them at their junction. At Dowa-
cima falls, on the Barama river, a green mica-schist occurs contain-
ing veins of granite. Chlorite-schist also appears in many places,
pierced by grey trap dykes. The same series of rocks occurs on
the Barima and Wainii; but those above tide-water are chiefly
gneissose, with small veins of quartz, or coarse granite, in which the
quartz is in semitransparent crystals an inch in length, and the fel-
spar of the same dimensions and of a milk-white colour, while the
mica is an inch and a half in diameter and half an inch thick.
My next excursion was along the western shore of the Essequebo,
then up the Cuyuni, to the line of Venezuela, then across the land
between the Cuyuni and the Puruni, a tributary of the Mazuruni,
and then up the Mazuruni towards the highest lands of the colony.
Dee
[May 24,
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Seale 104 miles to 1 inch.
u
|
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Fig. 1.—Sketch Map of the Geology of British Guiana.
ME Wael,
a
‘Rarauma
ar
Sandstone formation ...
Alluyium.....
Granite and Syeni
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SAWIKINS
1871. ]
On reaching the western shore
of the Essequebo, my course was
nearly south-west to Supinaam
Creek, which courses along the
base of the sand- hills to the Mis-
sion of Indiana, where these hills
rise nearly 50 feet and are com-
posed of sand and clay; decom-
posed granite, or gneiss-quartz,
occurs as aggregated pieces of con-
glomerate cemented by red or
white clay. Where the clays are
separated from sands, they are
mottled or streaked with red lines
of oxide of iron. Sand-deposits
increase in ascending the creek,
and occur in many instances with-
out any argillaceous admixture.
Above the Mission there are ra-
pids, near which the granite is
exposed, and numerous small is-
lands formed by deposits accumu-
lated on it.
In proceeding up the Groote
Creek, which runs parallel to the
Supinaam on the south, the same
series of granite rocks is exposed
here and there, and likewise along
the banks, under deposits of sand
and clay.
Saxacalli point is composed of
granite and appears to be the re-
mains of a dyke that extended
across the HEssequebo river. On
examination it was found that none
of the rocks composing this group
presented any sharp edges ; all are
rounded by attrition or disinte-
eration. The surface of the granite
is worn away below the quartz
veins that run through it; and al-
though they present no regula-
rity as by deposition, yet there is
such an amount of parallelism as
we frequently find in false bed-
ding of sand and gravel, while the
lines of separation in the granite
are more constant in one direction,
dividing the quartz veins as well
as the granite. At Swarte Point,
BRITISH GUIANA.
i
a)
Fig. 2.—Section from the Roraima Mountain to the Quitaro River.
A
eh ATES Ta STE EE (©) a
DS
Ze
se
As
TAO, UL gee St XIN
nynury eh SY
ie
th
BONGO ue oe eee SS
runundny K
i
NAIVUIIH -—--—-=————--—~ - I
Ht
i
“eB ~------———-—— Ik
*IOALY SUOT] —=-==----———— -
“TOATY
BlBUBU()
ed ae
‘IOAN
TpVAMIUoy §
“LOATY pe
eupdniedumg §
TOALY BUOVOVE-~--—————_.__ |
“AOTTV A.
SUBUBYBIE
cael
oF
eee
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aoe
pee
Ke
Be)
bas
N,
2
“LOATY BAULIYOD --—------__-
“ULBJUNO TL \
ndiqoB AA
“uUIBqUMOyy =.
BULIBLORT §
(For explanation see Map.)
Vertical Scale 10,000 feet to the inch. Horizontal scale 28 miles to the inch.
422 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
a few miles south, the same characteristics appear on a larger scale
in the granite, but in place of regular lines of separation a folia-
ccous structure predominates. At the penal settlement the land rises
56 feet; and this is the highest point on the lower portion of the
river Essequebo ; it is composed of a grey and red granite much de-
composed on the surface. Some quarrying that has been done here
presents good sections.
Almost immediately opposite the Commissioner’s House, on the
opposite side of the river, is an intrusive dyke of greenstone; and at
the mouth of the Mazuruni there is a large quarry of granite well
worthy of examination.
Proceeding up the Cuyuni, instead of going over the falls of
Seregatara, Tivrimi, and Ematubo, I walked across the land. The
rocks observed on this path are granite, syenite, and quartz, the
latter not in veins, but granulated. The same rocks occur above
the cataract of Camaria and on one of the numerous islands between
it and Woko Creek and Powis Hill, on which hydro-oxide of iron
and hematite, with quartz in detached pieces from 2 to 6 inches in
diameter, lie on red and variegated clay.
At Arnakanmatabo there is an intrusive hornblendic rock, asso-
ciated with granite, on the surface of which is ironstone, or hydro-
oxide of iron in the form of gravel, or cemented by clay into a stiff
conglomerate, a large block of which is lying at the mouth of a
small stream at the east end of the Tapore Hills. On the western
part of these hills there is a mass of quartz, about 200 feet in length,
and 25 in width, containing minute specks of gold, lying on de-
composed mica-schist, which has been mined in different directions
in the expectation of intersecting it. Had it been a vein, or reef,
it would have been intersected ; but it does not descend so far below
the surface as where the adits are driven.
About one mile and a half up the river, there is a rivulet, where
the mica-schist is more compact; and after washing the black sand
collected in the rivulet for some time I detected a few minute specks
of gold, which may have been derived from the adjoining rocks, but
most probably from those of the auriferous country at the head
sources of the river Cuyuni, where gold was collected by the natives
prior and subsequent to the discoveries of Columbus.
Proceeding up the river Cuyuni, syenite appears again at the
rapids on the south of Suwaraima Island, and at the extreme
north-west point of it in juxtaposition with an intrusive trap or
greenstone; these occur again about four miles further up the
river.
Near the Berebisi creek and Tonoma rapids, granite and syenite
occupy a considerable part of the river-bed ; they also appear at the
rapids of Payuca, and up as far as the island between the Quive
Kura river and the Zane Kura, at the extreme end of which there
is a body of quartz, around which a quantity of black sand is de-
posited. In this a speck or two of gold was found; but in the quartz
at this locality I could see no gold, even by the aid of a strong mag-
nifying power.
AST SAWKINS—BRITISH GUIANA. 423
After passing decomposed granite, syenite, and quartz, about a
mile below the Caruma creek, on the north, and the Wairyarra, on
the south, the rocks become decidedly schistose. There is also a
small dyke of quartz of a red and white colour in the course of the
river ; but by microscopic examination no gold could be seen in it.
At the base of one of the hills in the vicinity, gold in very small
quantities was soon obtained.
On passing over the rapids of Olupikai a variety of greenstone and
talcose-schist occurs, very slaty in structure, particularly at the
rapids of Atete, where it is of a greenish colour. :
At the cataract of Waicuri there is an extensive development of
the red brecciated rock lying on a phonolite, with small crystals of
pyrites, and a blackish mineral that, like the pyrites, dissolves out
of the rock, leaving square cavities more or less filled with oxide of
iron.
At the falls of Wakupany, the rocks are principally greenstone,
or coarse schist, on which there is a considerable deposit of white
sand. A little up the river the rocks become more slaty and foli-
aceous by the presence of talcose-schist with quartz veins 2 inches
in diameter, and a good deal of iron pyrites.
The granite rocks in the river from this point became more
gneissose, with occasional quartz veins; therefore the space between
the Copang and the Maruparu creeks may be regarded as the
schistose district on the Cuyuni river, within the boundary of
British Guiana.
From Maruparu taleose schist occupies a considerable portion
of the north bank. On approaching the falis of Duquari, the granite
rises in large bosses alternating with syenite, porphyry, greenstone,
and hornblendic and talcose schist, which lie on the granite at different
angles. Above the Iroma river, these rocks are more decomposed, and
assume a red colour, but still preserve their laminated structure.
At Duquari falls there is a better opportunity. of observing these
various rocks and determining their relative age. It appeared to
me evident that the greenstones have displaced the granite, and in-
truded through lines of weakness, or fissure, without materially
altering the granite, by which it also appears that the greenstone
was at a low temperature during its ejection, 2. ¢. below a white heat,
like the lava of the present day at Vesuvius, and at Mouna Loa,
in Hawaii.
From the Duquari falls to the Otomong river, granite is general,
except where the cataracts of Aroroyamo, Callo, Darra, Corrocoro-
roopung, Icarima, Poinchaima, Tacarric, and Aberiwaika traverse
the river by dykes of greenstone, gneiss, &e.
After passing the Paccu falls there is a small creek called Cartuni,
along the banks of which there is an Indian path that leads to the
Puruni, a tributary of the Mazuruni river, over which I made the
transit on foot. I estimated the distance to be twenty-one miles.
The rocks observed on the way were granite, granular quartz,
syenite, and trappe. In the creeks black sand occurred very gene-
rally ; and I consider this part of the Cuyuni valley at least as likely
424 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ May 24,
to contain auriferous deposits as any other portion of it that I
haye seen.
The greatest elevation between the Cuyuni and Puruni rivers
was 320 feet, on the south of which a tributary of the Puruni
takes its rise. Down this narrow stream, we cut our way through
the branches and trunks of trees that were lying across it. After
passing the Tapara and the Tariparu creeks, from the south, granite
and syenite occur in two places, and after passing the Waini creek,
from the north, the river is divided into many branches by nume-
rous islands composed of a red clay, and obstructed by fallen trees, to
avoid which the Indians have cut a passage through the clay, large
enough for corrials (canoes) to pass. These clay banks are generally
low, and lie on some hornblende and schistose rocks near Maruparu
and again further down the river.
Granite occurs near Tuvastimpi creek and a little below, associated
with gneiss of a blue colour.
On approaching Curaspara creek a soft mica-schist occurs, near
which there is a hill of 600 feet elevation. The ascent is rather steep
being on the average 30° of inclination; the trend is north-east,
and south-west. The surface is covered with hydro-oxide of iron,
in the form of pebbles, or in concretionary masses, sometimes con-
glomerated and heematitic.
Near the falls of Marchughi the hydro-oxide of iron occurs form-
ing a soft rock, with blackened surface. Diorite, trap, and green-
stone form the barrier across the river, about 15 feet higher than
the lower basin. A deposit of iron and manganese occurs on all the
rocks in this as in most of the other rivers in the colony. Some-
times I have seen it + of an inch thick.
About a quarter of a mile below the junction of the Mapa-aima
with the Puruni, are the falls of Payuca, which are divided into three
streams. A dyke of greenstone forms the obstruction. The mica-
schist dips to the south-east.
Ombaroa Creek enters the Puruni from the north a little below
these falls, and the hills of Ruminga and Murupina soon appear,
forming the south bank. At the base of these hills are dykes
of a dense greenstone. Between these two hills is a small water-
course, near which I observed granite, syenite, trap, hornblende-
schist and decomposed schist. Near Gasparupa creek there is a
curious conglomerate, and also trap with quartz veins. After
passing Gangrooma and Langooma creeks greenstone occurs; and
below Cabilli and Humaribara creeks quartz, greenstone, and con-
glomerate; and at Paraani creek red and green schist with quartz
veins. These extend down to the vicinity of the Maramara creek,
where gneiss and blue clay-slate appear. A short distance lower
down the river 1s a bed of conglomerate.
The river soon after passes through a ridge trending north-east
and south-west, and soon after another hill is seen about the same
height (600 feet) trending more to the south. Then follows the
Uricon, which is the highest in the range.
At the base of these hills a ferruginous conglomerate and red
187 1.] SAWKINS—BRITISH GUIANA. 495
clays are found accumulated on either granite or some hornblende
rock.
Near the Tacuparu creek a decomposed granite appears, also at
the rapids of Maritote, and others below them, where the granite
and syenite are extensively exposed.
After passing several rapids, including that of Alabamaloo, the
syenite is more general. A remarkable dyke of porphyry, 4 feet
wide, which has passed through the granite, occurs at the falls,
which were about 12 feet in height at the time I descended.
The granite series, with trap dykes, are more largely developed.
At Huamata they cross the entire river. Most of this granite is
very coarse-grained, with green or red felspar.
At the rapids and the island of Taparu, also at the rapids of
Presatu, white granite occurs; and near Cubangan, gneiss, which
extends down to the Ourasas-sartur rapids.
The land rises here, on each side of the river, to from 150 to 200
feet. At the base granite, syenite, trap, and quartzose rocks spread
out over amuch larger surface, in comparison with those on the upper
part of this river.
After passing the great falls at the junction of the Puruni with
the Mazuruni, there is so great an extent of bare granite separated
into innumerable islands, and such a large expanse of water within
the low and distant confines of the river, that it presents a scene
rarely to be met with.
On entering the Mazuruni I found the river unusually low, and
consequently many rocks exposed that would not have been seen had
the river been in flood; but all are so uniform in their character
(granite, syenite, gneiss, and porphyry, with trap dykes) as to
render the labours of the geologist very monotonous.
These rocks continue up the river without any important modi-
fication as far as the Wanamu and Maribisi rivers, where a fine
conglomerate occurs. Above this there is an altered sedimentary rock,
forming a mass.
At the falls of Tebuco there are granite, diorite, and very dark
porphyry, also veins of dark quartzite, followed by greenstone, and
schistose rock with quartz veins, both black and white.
At Carinang Creek the same rocks occur, and continue some
distance further up the river. Some of the quartz veins are bold,
being several feet across; but no gold could be detected in them with
the aid of a strong magnifying power.
About this part of the river I obtained the first view of the
Maribiacru cliffs, which form a part of the Meremé range, rising
from 1000 to 2000 feet over the forest-trees growing on the banks
of the river.
At a point turning south, towards the cliffs, granite underlies 8
and 10 feet of recent conglomerate and sand interstratified ; then the
granite again rises to the surface.
At this point the heights of Caribisi are seen to rise in a peak
about 18 to 20 miles distant; and not far above, conglomerate is
again seen lying on white granite with quartz veins. This is fol-
426 PROCEEDINGS OF THE GEOLOGICAL society. . [May 24,
lowed by greenstone of a greyish hue, forming a dyke in a N.E. and
S.W. direction, the rapids of Curanassai and a large gravel beach.
Beyond this point were observed gneiss, hornblende! trachytes with
iron pyrites, greenstone, a dark grey trap, quartzite followed by
greenstone, schist, porphyry, and altered conglomerate.
At the mouth of the Carubung river there is a talcose aie
through which there are small veins of plumbago or graphite; these
are followed on the Carubung river by gneiss, greenstone, porphyry,
granite, mica-schist, ironstone, conglomerate, sands, and clays.
Several precipitous cliffs of stratified rock appear here above the
forest, forming the Morokina, Wataparu, and Curumina mountains ;
and the granite and metamorphic series of rocks are occasionally
covered by large blocks of old conglomerate, composed of white
quartz pebbles in a very hard siliceous matrix, which lie in the
river at different angles of inclination. Soon after, the grey and
pink granite disappear under extensive beds of conglomerate, com-
posed “entirely of siliceous rocks or quartz pebbles and boulders,
coated, as all the rocks are in the rivers I have visited, by hydro-
oxide of iron, with or without manganese. The falls of Macrabah
are produced by a mass of this rock traversing the river 35 feet
between the level of the water above and that below.
The hills on either side of this river, at the Macrabah falls, rise
almost perpendicularly to the height of 13800 feet. ‘To gain the
summit, I proceeded up the Seronne, a smaller stream, and climbed
up over large masses of conglomerate and sand until I attained that
altitude.
By a slight divergence to the north of the Indian track a cascade
may be seen, reported by Hillhouse to be 400 feet perpendicular ;
it was dry when I passed.
On reaching the summit of that portion where the land becomes
comparatively level, I found it to be, by aneroid barometer,
1500 feet, continuing to rise in a distance of ten miles to 2534 feet
above the sea-level.
Nothing but sand (red, yellow, or white), ironstone, conglomerate,
quartz-pebbles, as white as milk, and greenstone dykes is to be
seen in the course of this transit.
On reaching the southern portion of this range I found it equally
precipitous, and was obliged to descend by the ‘aid of ropes tied to
the trees that grew scantily out of the mural side of about 700 feet
before reaching the level below.
The space between the base of the precipice and the Upper Mazu-
runi is occupied by rugged sand-hills cut by small streams into
deep ravines.
The alluvial banks of this part of the Mazuruni present the same
general aspect that they do below the great falls of Piamah, but
become narrower on arriving atits junction with the Cako. On this
part of the river granite was only observed at three points, under
either the old conglomerate or recent alluvium.
From the mouth of the Carubung, during the journey up the
Mazuruni, the rocks that appeared above ake surface of the water
HS aly SAWKINS—BRITISH GUIANA. 427
consisted of trap, trachyte with iron pyrites and red decomposed
pyrites, a greenish porphyry with quartz-veins, then trap and
diorite, mica-schist, quartz, and a very hard purple trap, form-
ing a dyke a little below the great falls of Piamah, which are now
cutting away beds of sandstone and conglomerate that present
escarpments like masonwork, so regular are the lines of stratifi-
cation.
This was the extent of my second excursion and examination on
the Mazuruni river. I estimated the distance from the coast to be
430 miles.
Examination of the River Demerara.
The lower portion of this river is exceedingly monotonous and
uninteresting, being formed of low alluvium from the coast up to
the ‘‘sandhills.” Between these two points there is little else than
swamp or low muddy flats covered by caladium, arborescent arums,
mangroves, &c., and affording not even a landing-place of sufficient
firmness to support a man.
The sand-hills are low and undulating, composed chiefly of a
whitish sand with a little clay ; they rise a little as they recede from
the river, but nowhere exceed the height of 70 feet, until we arrive
at Berlin.
At Dalgnin the hills rise higher, but none so much as 200 feet,
until near Christianburg, where the country becomes decidedly
hilly. About two miles above this the first rock, a coarse-grained
trap, is seen near the centre of the river at low tide.
At Akyma one of these hills has been cleared of timber, and gives
an opportunity of seeing the configuration of the surrounding
country. To the east and south the land is low and swampy, and
is often overflowed by the river.
At Seba a boss of granite (common) rises from 15 to 18 feet on the
east side of the river, exposing an area of more than fifty yards; and
at Tiger’s-leap, on a hill about 350 feet high, some large boulders of
granite occur.
The sand-hills seldom rise over 300 feet ; on one near Manabadin
there is a landslip or breakaway, by which the lines of stratification
are seen resting on granite.
At the rapids of Mouranicrocaba the granitoid schist constitutes
the barrier across the river, forming rapids and falls of 5 or 6 feet
perpendicular.
At Labacabra granite appears, and continues up the river as far as
Curuwa creek, where a fine-grained hornblende rock occurs; the
same appears at Curabelicabra, also at Morocabra, and occasionally as
high as Arampa, where sand and clay compose the banks. At the
base of a hill near Umpa a white pottery-clay forms a bold bank.
At the north of the next creek, Cornbara, there is an island com-
posed entirely of sand. About two miles further up there is a hill
covered chiefly with hydro-oxide of iron, bearing the appearance, in
some instances, of cellular lava or scorie from a furnace. This same
formation crosses the river near Couchman’s grant, where the river
428 PROCEEDINGS OF THE GEOLOGICAL SOCIELY. [May 24,
is very shallow by the accumulation of this ferruginous gravel. At
the base of Mecropie hill the same occurs.
Derrire hill is covered with hydro-oxide of iron; and much of it has
been brought down, in the form of gravel, into the creek bearing the
same name.
At Camoodecabra a trap rock rises, and extends to the Anobaro
Creek, forming a dangerous barrier for boats descending the river.
Above the Waburicabra another large ferruginous gravel-bank occurs
that extends up almost as far as Coomaparo creek.
From Coomaparo there is an Indian path to the Hssequebo river,
which occupied eight hours’ walking. ‘The land rises in undulating
swells up to the “burnt grounds, where it attains 200 feet, and,
after continuing on that level for a few miles, gradually descends,
like steps, until it reaches the low swampy flat of Moraboo, on the
east bank of the Essequebo.
In this distance, computed at 18 miles, the only rock to be seen is
a quartzite, which decomposes into white sand.
Returning to the Demerara river, the banks continue low until
arriving at Acururi Hill, which connects with a ridge that extends to
Lucananycabra, chiefly composed of white sand.
By proceeding up the Marbooroo creek about a mile, and then
walking south-west a few miles, the Maburu Hill rises to about
800 feet above the sea: one of its sides towards the Essequebo is
nearly perpendicular; and from it a fine view of that river is
obtained. It is composed of trap, and appears connected with the
same range that forms the dyke at the great falls of Malalli.
The falls of Malalli are 35 feet in perpendicular height, and form
the greatest barrier to the navigation of the Demerara river.
At the base of the falls may be seen ejections of trap and por-
phyry between the granite; and on the confines of the basin below
the falls, several iiperesanne examples of weathering and decom-
position of the granite.
The trap or “ereenstone, that has passed up the fissures or lines
of weakness, appears very dense, and so fine-grained that it might
be taken for petrosilex. The curious puma neti: and the splitting
of veins that have forced their way through masses of granite are
exceedingly interesting and instructive.
The hornblendic rocks continue over a distance of ten miles up
the river, occasionally rising to the surface, but more frequently
observed covered by clays and sands, resulting from the decompo-
sition of these and granitic rocks.
Where the clays or sands form the banks of the river the land is
low and often swampy for miles around, intersected by numerous
bayous, showing a considerable depression of the country.
On approaching Navaroo creek, granite occurs of a very beautiful
character, with purplish felspar and green mica.
There are several large boulders near Kanimapoo’s Landing.
This series ‘of granite continues up the river four or five miles. ‘A
very good yellow- ochre appears to be the result of its decomposition,
and occurs in thick beds in this vicinity.
1871.] SAWKINS—BRITISH GUIANA. 429
Arriving at Uriburoo Hill there is a bold escarpment of trap
and schist, with iron pyrites. A stream runs down the cliff, as a
cascade, on the west side of the river. On each side of the river, as
high as the Ubaroo creek, trap dykes occur traversing the river;
and between these is a ferruginous gravel, sand, or clay. The land
beyond this is low and swampy, and traversable only during the dry
seasons.
Observations made on the Essequebo River, its tributaries, and
southern mountain-ranges.
At the junction of the Mazuruni and Cayuni rivers with the
Essequebo is the penal settlement, and on the opposite shore the
village of Bartica, the only settlements of civilization on these rivers ;
and as the geology between this point and the sea has been already
given, I commence the following observations from Bartica, which
is built on a low sandy deposit resting on granite and porphyry.
This low land continues to the cataract of Aretaka; but before
arriving at Camaka Serima, dikes of greyish trap with iron pyrites
and felspathic hornblende occur. At Camaka Serima grey granite,
somewhat gneissic, rises, dividing the river by several islands and
forming the Aretaka cataract, where the granite appears in large bold
masses, sometimes showing lines of scaling or peeling in concentric
layers like an onion, at others of decided gneissic structure. The
entire area occupied by these falls or cataracts is composed either of
granite proper or of members of the granitic family ; at the head of
them is Gluck Island, and a great extent of still water expanding
to lacustrine dimensions, where no rock is seen im situ, but large
sand-banks render the water very shallow.
A few miles up the river the Arissara hills appear ; and near their
base granite occurs; and a little up the river a trap dyke crosses
it.
From this, for several miles, nothing but sand and clay is seen.
At the Cumuka rapids, granite with quartz-veins 2 inches in dia-
meter appears, with detached blocks of hornblendic rocks superposed.
At Acuramalli Rapids trap rocks rise a few feet above the river,
also at those of Curamucu, where greenstone and hornblendic rocks
form obstructions in the river.
A short distance above this are the hills and islands of Buhuri
and Banaca, and the Waraputa falls, where the granite extends across
the river, some of it being very dark from the quantity of black
mica it contains. There are veins of quartz a few inches in dia-
meter, also petrosilex, gneiss, and syenite, diffused much in the same
manner as at the Malalli falls on the Demerara river, with which
this is in all probability connected. A depression in the land to the
south-east also corresponds with that on the Demerara river.
After passing the next rapid there is a collection of granite rocks,
all having a scattered and confused position detached from each
other, some larger ones on smaller. To one of these the name of
Paiwori Cayra is given by the natives, from its resemblance to the
430 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
vessel in which they preserve their favourite liquor “ Paiwori;” it
resembles some of the rocking-stones.
After passing the still water in the depression mentioned I came
to a succession of rapids rushing and pitching over beds of granite
and dykes of trap that traversed the river, until I arrived above
the falls of Itamine; soon after the Taquiari mountains came into
view, about 800 feet above the river. i
This is the first place where I observed sandstone in situ; dykes of
greenstone pass through it, and rise on the south-east side of the
Taquiari. At the termination of the hill, about 600 feet above the
river, a column of rock stands out from a somewhat similar one, which
makes the final point on the hill. This has weathered into three
distinct pieces of rock, resting on a broad base one above the other.
At each junction there is a separation ; and as at these junctions the
weathering of the rock has been greatest, each piece has assumed a
spherical or elliptic form; and as the difference in size of the three
is proportionate to the form.of the large water-vessel used by the
natives, the name ‘“Comuti” has been given to it by the Araa-
wak Indians and “'Taquiari” by the Caribs, both signifying a large
water-jar.
South of these hills there is a great depression or extent of level
land towards the south-east, corresponding to that I observed at the
upper part of the Demerara river. The banks of this river are low;
and, I suppose, by a rise of ten feet above the present level it would
overflow its banks. Before reaching the large pond of Tambicabo I
observed some altered sandstone in the middle of the river, the
granular structure of which is nearly obliterated, making it appear
like flint: it decomposes into white sand.
The Tarratara hills are seen in the distance; the land around
them is low, extending apparently many miles back from the river.
At the falls of Ouropocari there are some very curiously water-
worn rocks; parts of them are porphyritic, and others like an
altered conglomerate. They are deeply grooved by weathering ;
some rest on others of very inferior size, leaving space beneath them
to shelter many men.
After passing over a series of rapids and cataracts formed by
dykes of trap and porphyritic rocks, the Macari Mountain is seen, ©
with a mural precipitous escarpment of near 1000 feet above the
river. The range appears to trend off to the S.E.; the summit is
comparatively level, resembling the sandstone mountains on the Ma-
zuruni river ; and it appears to have been cut away by the Essequebo
river, but resembles more the cliff of a sea-coast. At the base there
are dykes of a purple-coloured porphyry.
At the Pishani falls the rocks present the character of altered
sandstone. At the upper part of the falls these rocks are of much
finer grain.
On the east side of the river, granite rises to the surface and covers
a considerable area, particularly at the cataract of Achramucra.
From this the river rises but little, as it becomes comparatively still
water.
1871.] SAWKINS——BRITISH GUIANA, 431
From this no rocks appear above the surface until arriving at
“« Musara,”’ an abandoned Carib settlement; and from this to King
William IV. Falls, a distance of five days from this point, there are
no rocks to be seen but granite, syenite, gneiss, a series of dense
hornblendic rocks, and in one instance columnar basalt.
The Falls of King William IV. consist of a succession of rapids
about 100 yards apart, closely interspersed with rocks.
The Ascent of the Rupununt.
The Rupununi river is one of the largest tributaries of the Esse-
quebo, entering it at nearly 4° N. latitude; there is scarcely any
current perceptible at their junction; and high banks of alluvium
occupy both sides of the river, which are sometimes broken by large
ponds or inlets, conveying the idea of an extensive depression be-
tween the Maccari and Paccarima ranges, and again between the
Makrapan and the Annai.
The Makrapan Mountain is composed of granite and syenite.
From the base of this mountain} the great savannas spread to the
south and west into Brazil and Venezuela like large inland lakes,
a resemblance which is increased by the difference of vegetation
growing on them. The alluvial deposits of the lower Essequebo are
covered by the largest and highest forests in the world, whereas on
approaching these savannas trees begin to decrease in altitude
until they become like the stunted growth on a promontory of a sea-
coast. This peculiarity is not confined to the river-courses; for
the savannas or grassy plains are only here and there dotted by a
dwarf tree resembling the coast-grape, Coccoloba wvifera.
The geology of these savannas is very clearly defined, as they con-
sist of only three distinct, stratified Tertiary deposits, resulting from
the disintegration of the adjacent mountains :—1st, sand, clays, and
vegetable mould; 2nd, red sand and ferruginous gravel, often con-
ereted or hematitic; 3rd, white clay, resting on gneiss, granite, &c.
On the Annai mountains the savannas, or tracks of land denuded
of trees, rise to the summit in a most capricious manner in strips and
lines as regular as if laid down by line and compass ; but the rocks
do not differ in character from those on which forests grow.
To the south of the Paccarima or Annai range are the Cunuku
mountains, which extend from the Takutu river on the west to the
upper Essequebo. This range is chiefly composed of granite and
oneiss, with trap dykes of the same character as those before de-
scribed. The savanna from the Rupununi to the Ireng and the
base of the Paccarima mountains consists of three Tertiary stratified
deposits. At the mouth of the Unamara river there is a vein of
quartz, and adjoining it are hills of quartz similar to those of Annai.
Between the savanna and the Unamara river there is a ridge of
granite intersected by greenstone dykes.
The next hill to the northward is composed of a different kind of
rock, which continues to the edge of the sandstone escarpment on the
Sacaonta river. This rock in its commonest form is composed of
white crystals of felspar and clear crystals of quartz in a siliceous
432 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 24,
base of extreme hardness ; it usually contains crystals of hornblende,
and occurs in regular layers of great thickness, some of which are
massive and break with a conchoidal fracture, while the others are
slaty and split vertically. It often occurs in isolated patches in the
valley and Unamara river. Although this rock has been called and
laid down on the map as quartz-porphyry, I should rather regard it as
an altered sandstone or quartzite, as by further investigation I found
the lines of stratification sufficiently distinct to justify such an in-
ference.
Large dykes of greenstone occur, similar to those in granite, tra-
versing this formation, which extends to the Marakang river, where
it passes under an escarpment from the top of which sandstone like
that observed in the Mazuruni and Carubung has rolled down. At the
base of the hill a greenish bedded rock, dipping north, with green-
stone dykes and quartz veins, lies upon the conglomerate and white
quartzose sandstone, occupying in vertical height some hundreds of
feet; and upon these are beds of considerable thickness of red and
yellowish sandstone ; the latter are slightly contorted.
Continuing up the valley of Murapang the stratigraphical arrange-
ment is as follows:
Grey sandstone in thin beds.
Yellow sandstone.
Pinkish sandstone.
White hard sandstone.
Conglomerate, dipping from 5° to 10° N.
Strike of the hill N.W. and S.E.
Not far from the Karakanang river there are low rounded hills of
white and pink argillaceous sandstone, on the surface of which
quartz crystals occur in such quantity that they are called Crystal
Mountains.
The mountain to the north-west of the village presents the fol-
lowing section :—
150 feet: of dark green slaty rock resting on granite.
175 ~,,_~—red shaly sandstone.
175 ,, hard white quartzose sandstone.
100 ., coarse pebbly conglomerate.
200 ,, pink and grey interbedded argillaceous sandstone.
100 _,, _ red ferruginous sandstone and beds of red jasper.
The hills beyond the Karakanang river are formed of the white
argillaceous sandstone with small water-worn pebbles of quartz &c.,
on which lie beds of hard red jaspideous sandstone.
Beyond the Peepee river to the Cotinga a red thin-bedded sand-
stone occurs, containing red jasper; and at the falls of Orinedouke,
on the Cotinga also ; and from that to the pyramidical mountain of
Waetipu and Roraima, the sandstone forms the surface-rock.
Waetipu mountain is composed of horizontal beds of sandstone and
conglomerate of a light yellowish or grey colour. Height estimated
at 5000 feet.
Roraima is a flat-topped mural mountain, rising to the height of
7500 feet above the sea, with + perpendicular wails’ of 1500 to 2000
1871.] SAWKINS-——BRITISH GUIANA. 433
feet from the summit to the inclined portion surrounding it like a
glacis or closely built buttresses, and formed by accumulated débris.
This and the surrounding mountains are composed of sandstone
and conglomerate resting on gneiss or granite, with intrusive dykes
of greenstone &c. When we consider that not a fossil of any kind
has been discovered or limestone in any form, and also the fact
already ascertained of the extension of this formation from Venezuela
to Brazil, and perhaps to Patagonia, it becomes an object of great
interest.
Schomburgk speaks of the sandstone range of Humerida to the
south of Roraima and of the sandstone of which Fort Sao Joaquim
is built on the Rio Branco, 2° south. Travellers on the Amazons
speak of flat sandstone mountains as called by the natives “Guiana
Mountains ;” and from Darwin’s observations on the more recent
formations of the valley of St. Crux, in Patagonia, I infer that
Roraima represents deposits from the Cordilleras at an earlier
date and under similar conditions, and since it was uplifted it has
been eroded by the waters of the valleys of the Essequebo and
Orinoco.
Returning to the extensive granite and gneiss formations, there is
on the Rewa, a tributary of the Rupununi, a ridge of granite which
presents several conical or pyramidal hills, one of which, Ataraipu
or Devil’s Rock, is nearly bare of vegetation, and rises about 900 feet
above the river and 550 feet above the forest by which it is sur-
rounded; it is south-east of Roraima, and forms a part of the
Cunuku range.
Discussion.
Prof. Ramsay remarked upon the barrenness, from a geological
point of view, of the district investigated by Mr. Sawkins, and
especially called attention to the absence of fossils in the stratified
rocks. He referred briefly to Mr. Sawkins’s labours in Trinidad and
Jamaica, and to his discovery of metamorphosed Miocene rocks in
the latter colony exactly analogous to the metamorphic Eocene
rocks of the Alps. He was glad to see that the author had brought
forward examples of cross-bedding in metamorphic rocks, and con-
sidered that the results adduced were favourable to those views of
the metamorphic origin of granite which he had himself so long
upheld.
Mr. D. Forszs, on the contrary, considered that the facts brought
forward by Mr. Sawkins were confirmatory of the eruptive nature
of the granites observed. He added that a structure analogous to
the so-called cross-bedding was common in igneous rocks and even
in lavas.
Mr. Tarr remarked that in the country to the north of the dis-
trict described in the paper metamorphic rocks abound. He con-
sidered that the series of metamorphosed Jurassic rocks extends
across the whole north of South America, and perhaps into Cali-
fornia. Similar sandstones to those described occur in the basin of
the Orinoco, and contain fossils which show them to be of Miocene
VOL. XXVII.— PART I. 28
434 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 7,
age. Mr. Tate did not consider these sandstones the equivalent
of the Patagonian sandstones, as the latter, from the shells con-
tained in them, would appear to be Pliocene or Pleistocene.
Mr. Sawsrys, in reply to a question from Mr. Tate, stated that
the only gold found in the country had probably been carried down
from the well-known gold-district of Upata. He also entered into
a few additional details connected with the chief points in his paper,
dwelling especially upon the physical features of the country, in
illustration of which several landscape drawings were exhibited.
June 7, 1871.
Henry Collinson, Esq., 7 Devonshire Place, Portland Place, W.,
and Thomas Milnes Favell, Esq., of Highton College, Gateshead,
were elected Fellows, and Dr. J. J. Kaup, of Darmstadt, was elected
a Foreign Member of the Society.
The following communications were read :—
1. On the Persistence of CARYOPHYLIIA CYLINDRACEA, Reuss, sp., a
Cretaceous Species of Coral,in the Coral fauna of the Deep Sea.
By P. Martin Donean, M.B. Lond., F.R.S., F.G.8., Professor of
Geology in King’s College, London.-
TE simple stony coral Caryophyllia cylindracea, Reuss, sp., is, com-
paratively speaking, a common fossil in the White Chalk.
Lonsdale described the form, under the name of Monocarya centralis,
in Dixon’s ‘ Geol. of Sussex,’ 1850; but it appears that MM. Milne-
Edwards and J. Haime had already named the species Cyathina
levigata in their Monographie des Turbinolides, ‘ Ann. des Sci. Nat.’
3° série, t. ix. p. 290, 1848.
D’Orbigny recognized the species in 1850 as a form which had
been described by Reuss in 1846 under the name of Anthophyllum
cylindraceum (‘ Kreideformation,’ p. 61, pl. 14. figs. 23-30); and
after altering the generic title, he created that of Cyathina cylin-
dracea.
MM. Milne-Edwards and Jules Haime described the coral in their
monograph of the British Fossil Corals (Paleontog. Society, 1850)
under the name Cyathina levigata, and, after recognizing the pri-
ority of Reuss in their ‘ Hist. Nat. des Coralliaires,’ finally accepted
the name of Caryophyllia cylindracea, Reuss, sp.
I have referred to the species in the Supplement to the ‘ British
Fossil Corals’ (Paleentog. Soc.) and in the Report on the British
Fossil Corals to the British Association.
Hitherto Caryophyllia cylindracea, Reuss, has been considered a
characteristic fossil of the White Chalk; and its horizon does not
appear to have reached that of the uppermost beds of that series.
1
:
1871.] DUNCAN-—PERSISTENCE OF CARYOPHYLLIA CYLINDRACEA. 435
The following diagnosis of the species was published by MM.
Milne-Edwards and Jules Haime in their last work, the ‘ Histoire
Naturelle des Coralliaires,’ vol. ii. p. 19 :—
“The corallum is elongate and subcylindrical, straight or slightly
curved ; the lower two-thirds of the wall are smooth and glistening,
but in the upper third there are small subequal and very slightly
prominent coste. The calice is subcircular. The columella is fasci-
culate, and is composed of a small number of delicate ‘ tigelles.’
There are four cycles of septa; but in the halves of three systems
the septa of the fourth and fifth orders are absent. The septa are
thin, but externally they are slightly thickened. The pali are narrow
and thick.”
An examination of a series of forms referable to this species
proves the general correctness of this diagnosis; but still it is not
sufficiently exact. Some rather important structural details, which
were noticed by these careful naturalists in their ‘ Monograph of the
British Fossil Corals’ (Pal. Soc.), are not contained in the above
diagnosis, and yet they certainly should have been. For instance,
the spreading base of the corallum narrowing rapidly into a more
or less cylindrical stem, and the occasional perfection of the
fourth cycle in all the six systems, are details which cannot be
overlooked.
It is quite true that corals with broad bases may become detached
above the base, and that they then possess a pedunculate appear-
ance; but the presence of a broad base is a positive structural
peculiarity.
’ The occasional perfection of the fourth cycle has not been ob-
served by me; but it is consistent with the variability of the septal
arrangement in other species in which irregular septal systems
prevail.
The distinctive structural peculiarities of Caryophylha cylindracea _
are the general shape, the condition of the wall, the development of
the costa, and the septal arrangement.
Caryophyllie with four cycles of septa complete in each of six
systems, and with the incomplete arrangement noticed in the spe-
cies under consideration, were formerly supposed to be extinct, and
to have been restricted to the Cretaceous and Tertiary periods. The
following are species with four perfect cycles :—
Caryophyllia Bowerbanki, Rd. & H., found in the Gault.
5 Debeyana, Ed. & H., from the Chalk of Aix-la-Chapelle,
ns Bredai, Ed. & H., from the Maestricht Chalk.
cylindrica, "Ed. & H.. from the Maestricht Chalk.
a Haine, Ed. & H., from the Maestricht Chalk.
Sismondai, Ed. & H., Turin Miocene, Sicily.
arcuata, Ed. & H., Older and Newer Pliocene.
Seguenza has, moreover, described many species with the four
eycles fully developed from the Older Pliocene of Sicily.
A species with the same septal arrangement has been found in
the volcanic sands of Guadaloupe.
2H 2
436 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [June 7,
The following are species with the fourth cycle incomplete :—
Caryophyllia cylindracea*, Reuss, sp. Wiltshire, Kent, Norfolk,
Chalk, upper beds usually.
Nehon (Manche).
Bilin and Weiss Kerchlitz.
is Lonsdalei, Duncan Dunstable.
The progress of research, especially in the investigations concern-
ing the fauna of the deep sea, has shown that there are some re-
markable exceptions to this rather hasty generalization.
Pourtales described Caryophyllia formosa, Pourt., in the ‘ Contri-
butions to the Fauna of the Gulf-stream at Great Depths,’ No. 6
(Bull. of the Museum of Comp. Zoology, Cambridge, U.S. 1868).
This form was dredged up off Havana in 270 fathoms. It has four
complete cycles in six systems. Although I have not seen the spe-
cimen, still I can but recognize, from the very able. description, the
decided fossil facies, if such a term may be tolerated, of the species.
During the last expedition of H.M.S. ‘ Porcupine’ +, under the
direction of Dr. Carpenter, F.R.S., and Mr. J. Gwyn Jeffreys, F.R.S.,
many specimens of Caryophyllie belonging to several species were
dredged up, some of which presented the perfect and others the im-
perfect development of the fourth cycle. Some species to which
they could be referred had hitherto been recognized as extinct forms ;
and others were new to science. Thus Caryophyllia arcuata, Kd.
& H., a well-known Pliccene form, was found not to be an uncommon
inhabitant of the deep sea; and Caryophylha abyssorum, Duncan,
a new species, was discovered in a dredging from the depth of 1095
fathoms off the coast of Portugal.
The falsity of the generalization which would restrict the Caryo-
phyllie with four cycles to extinct forms having been proved, it be-
came necessary to compare the forms dredged up from great depths,
and which had only four complete or incomplete cycles of septa, with
the fossil forms possessing similar arrangements.
I was especially led to do this on account of my having detected
some instances of remarkable persistence of form during some late
examinations of large series of corals from different formations.
Whilst I was impressed with the great variability of the reef-
building species of corals, and had obtained proofs of their increase of
variation under alterations in the surrounding physical conditions, I
became aware of the very persistent character and less variable
nature of the corals of the deep-sea fauna.
During the examination of the corals dredged up from the
Channel slope in 690 fathoms (No. 9 dredging, see Messrs. Carpen-
* Duchassaing (Anim. Rad. des Antilles, p. 15) described a species with an
irregular septal arrangement, but which is associated by MM. Milne-Edwards
and Jules Haime with the Caryophyllig having the incomplete fourth cycle ;
but an examination of the plate (Hist. Nat. des Corall. plate D 1, fig. 1) proves
that there are four complete cycles and part of a fifth, or else that the specimen
is a monstrous form haying seven systems. For a corresponding monstrosity
see P. M. Duncan, Ann. & Mag. Nat. Hist. 1865, vol. xv. p. 276, pl. xi. fig. 2, e.
t My description of the stony corals dredged up in the expedition of H.M.S.
‘ Porcupine’ is about to be published by the Zoological Society.
1871.] DUNCAN—PERSISTENCE OF CARYOPHYLLIA CYLINDRACEA. 437
ter and Jeffreys’s ‘‘ Deep-sea Researches,” Proc. Roy. Soc. Dee. 8,
1870) some Caryophyllie were noticed which possessed four incom-
plete cycles of septa, large and thick pali, and a columella made up
of from two to six processes. They had glistening walls; and the
coste were subequal and principally visible superiorly. They were
of course associated by me with the species cylindracea as varieties,
the variation being in the size of the pali and the number of the
columellar tigelles, both being very uncertain anatomical elements.
The dredging in 1095 fathoms off the coastof Portugal which yielded
Pentacrinus Wyville-Thomsoni, Jeffreys, produced many corals ; and
the series presented an eminently Cretaceous facies. The genus Ba-
thycyathus, whose species Sowerbyi is so well known in the Upper
Greensand, was represented there by numerous specimens of a species
closely allied to that form.
A new species, Caryophyllia abyssorum, was also found, which is
allied by its structural peculiarities to Caryophyllia Bowerbanki of
the Gault ; and the specimen was discovered which is the subject
of this communication.
The characteristics of Caryophyllia cylindracea, Reuss, sp., are
shown in the specimen in a most unmistakable manner. The type
is somewhat variable, and I have delineated some varieties in the
“‘ Supplement to the British Fossil Corals ” (Pal. Soc.); but the spe-
cimen obtained from the greatest depth at which coral-life is as yet
known to exist, belongs not to a variety, but to the original specific
type.
The interest of this proof of the persistence of a deep-sea coral
species is enhanced by its being associated with other corals which
possess Cretaceous alliances. The group of forms has a decided
Cretaceous facies. :
When the discovery of Caryophyllia formosa, Pourtales, and that
of the variety of Caryophyllia cylindracea, Reuss, sp., already alluded
to, are considered in relation to the small group from the great depths,
the homotaxis of part of the coral fauna of the Atlantic and that of
the Cretaceous ocean about the same area becomes very remarkable.
Such Cretaceous genera as Trochosmiha, Parasmalia, Synhelia, and
Diblasus are extinct ; but Amphihelia ramea, Mull. sp., represents
the Synhelie, and the position of the first two groups is now occupied
by species of Paracyatht and Caryophyllic, more elaborately con-
structed types, it is true, but adapted to the same bathymetrical
zones and for the same destiny.
Why such species as Caryophyllia cylindracea should persist, and
others, like Parasmilia centralis of the Chalk die out, is inexplicable,
unless it is admitted that there is a law regulating the life-duration
of species like that which restricts the years of the individual; for
the forms apparently throve under the same external conditions ;
and if these have lasted so that the one species has persisted gene-
ration after generation, how upon any other theory can the other
have become extinct ?
Considering that the generalization respecting the structural dis-
tinctions of deep-sea and reef-building corals must be accepted, it
438 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 7,
follows that deep-sea conditions must have prevailed within the limits
of the diffusion of the ova of coral polypes somewhere or other on the
Atlantic area ever since the Cretaceous period. The deposits which
were formed during the Eocene period in clear deep oceanic water
far off from coral-rerfs and muddy rivers have not been discovered ;
consequently the oceanic corals of the period are still unknown.
The muddy sea-deposits and the vast aggregations of reef-corals and
Nummulites so almost invariably associated abound; andin the Py-
renees and in the Hala mountains of Sindh there are littoral and
shallow sea-corals found with Nummulites. These last-mentioned
deposits and those of the London clay and Paris basin present evi-
dences of the existence of neighbouring deep seas as yet unnoticed
geologically.
I have already advanced, in former communications, proofs that
the reefs of the Miocene age of Europe were continued across the
Atlantic, through the Caribbean Sea, and into the great ocean-desert
of the eastern Pacific when the Isthmus of Panama and vast tracts
of land to the north and south of it were sea-floors. According to
the theory which distinguishes between the deep-sea and reef-build-
ing corals, the descendants of the Cretaceous oceanic forms could not
be found on the remains of that belt of islands which are to be traced
in the West Indies, the Faluns and away to the east far past Vienna,
and along the Italian peninsula. In fact, they have not been dis-
covered in those deposits.
But with the first evidences of deposits far from reefs and well
adapted for the invertebrate life of the deep sea come the proofs of
the persistence of deep-sea coral forms. The older Pliocene of Sicily
(the Zanclean of Seguenza) yields Caryophyllie with four cycles, and
species with shapes like those of the former deep seas, although with
important structural distinctions.
At the present time in the deepest known coralliferous depths of
the eastern Atlantic the persistent species, its varieties, and the
representatives of its former associates are living in consequence of
the resumption of the external conditions which favoured their ex-
istence before the initiation of the great alterations in the relative
level of the land and sea which destroyed the majority of the Cre-
taceous forms on the European areas before the age of Nummulites.
It is unnecessary to enlarge upon this part of the subject, as it has
been so ably handled by the President in his last Address; and it
therefore remains for me to conclude this communication by remind-
ing the Society that I have attempted to show that deep-sea corals
may persist somewhere through the ages when littoral and reef- and
muddy deposits were formed in their proper area, and may return
upon the resumption of the former physical conditions.
Discussion.
Mr. Gwyn Jrrrreys remembered that at the spot where the coral
in question was dredged up the sea-bottom was extremely uneven,
varying as much as 300 fathoms within a quarter of a mile. It
1871.] DUNCAN—PERSISTENCE OF CARYOPHYLLIA CYLINDRACEA. 439
was also not more than forty miles from land. The species of Mol-
lusca also procured in this dredging were extremely remarkable, and
many were quite new to him. They were, however, living or recent
species ; none of them were Eocene or Miocene, much less Cretaceous,
like TYerebratula caput-serpentis. He quoted from Mr. Davidson
instances of the persistence of Brachiopoda, especially of the genus
Lingula from the Silurian formation: The continuance of this species
of coral, as well as of certain Foraminifera, from the Cretaceous to
the present time was therefore not exceptional ; and other cases of
survival from even earlier times might eventually be recognized.
Dr. Carpenter, after commenting on the reductions that extended
knowledge enabled naturalists to make in the number of presumed
species, could not accept the mere identification of species as of the
highest importance in connecting the Cretaceous fauna with that of
our own day. The identity of genera was, in his opinion, of far
more importance. He instanced Hchinothuria and Khizocrinus
as preserving types identically the same as those of a remote
period, and as illustrating the continuity of the deep-sea fauna from
Cretaceous times. The chemical and organic constitution of the
deep-sea bottom of the present day was also singularly analogous
to that of the Chalk sea. The low temperature at the bottom of
the deep sea, even in equatorial regions, was now becoming univer-
sally recognized ; and this temperature must have had an important
bearing on the animal life at the sea-bottom.
Prof. Ramsay thought that there was some misapprehension
abroad as to the views held by geologists as to continuity of condi-
tions. They had, however, always insisted on there having been an
average amount of sea and land during all time; and the fact of sea
having occupied what is now the middle of the Atlantic since Creta-
ceous time would create no surprise among them. If, however, the
bed of the Atlantic were raised, though probably many Cretaceous
genera, and even species, might be found, there would on the whole
be a very marked difference between these Atlantic beds and those
of the Chalk. ’
Mr. Seetey had already, in 1862, put forward views which had
now been fully borne out by recent investigation. His conviction
was that, from the genera having persisted for so long a time, the
genera found in any formation afforded no safe guide as to its age,
unless there were evidence of their having since those formations
become extinct.
Mr. Erueringr maintained that the species in different formations
were sufficiently distinct, though the genera might be the same.
Recent dredgings had not brought to light any of the characteristic
molluscan forms of the Cretaceous time; and it would be of great
importance to compare the results of future operations with the old
Cretaceous deep-sea fauna.
Prof. Rurrrr Jones, with reference to the supposed sudden ex-
tinction of chambered Cephalopods, remarked that Cretaceous forms
had already been discovered in Tertiary beds in North America, and
also that cold currents could not have destroyed them, seeing that
icebergs came down to the latitude of Croydon in the Chalk sea.
440 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 7,
2.. Note on an IcutHyosavrvs (I. ENTHEKIODON) from KIMMERIDGE
Bay, Dorszer. By J. W. Hurxs, Esq., F.R.S., F.G.S.
[Puate XVII.]
On the 22nd December, 1869, I brought under the notice of the
Society two fragments of a long, slender snout with sauroid teeth
of a peculiar form, obtained in Kimmeridge Bay by J. C. Mansel, Esq.,
F.G.S., which I was inclined to refer to the genus Ichthyosaurus ;
but the evidence not being quite decisive I was obliged to leave the
true position of the Saurian indicated by them to be determined at
some future time, whenever new material for the purpose might
acerue. Meanwhile I gave it the provisional name Hnthekiodon,
from the thick capsule of cementum surrounding the tooth-fang.
A very few days afterwards, while making a short visit with Mr.
Mansel to Kimmeridge Bay, we discovered great part of the skeleton
of an indubitable Jchthyosaurus, the snout and teeth of which agreed
so closely with those of Hnthekiodon as to leave no reasonable doubt
of their identity, Mr. Mansel generously added it to the splendid
series of Kimmeridge fossils already presented by him to the British
Museum, and it has lately been placed in the Paleontological
Gallery.
The skeleton lies (as we found it on the reef) on its left side; the
head is bent upwards, the vertebral column makes a double curve,
the greater part of the tail is missing, a large number of the ribs on
the right side preserve their relations to the vertebral column and
to one another nearly undisturbed ; beneath them is a black stain
(cuttle-ink ?), in which are small scales; below the early thoracic
ribs lie the bones of the breast-girdle. The least mutilated fore-
paddle was inadvertently taken from the situation where I saw it
before the skeleton was removed by the quarrymen; and it and the
remaining hind paddle have been fixed in the slab below the
skeleton.
The anatomical details of the skull are not decipherable ; but the
orbit is large, and the eyeball has the usual bony ring.
The entire length of the head is 23-5 inches. The jaws are very
long and slender. “The teeth are smooth, slender, cylindrical,
and pointed; they are composed of an internal core of simple tubu-
lar dentine, the crown overlaid with enamel, and the root enveloped
in a thick smooth sheath of vascular cementum, which gives it a
bulbous figure. The basal end of the cylinder of dentine contracts
slightly, and it is also slightly and irregularly indented, very faintly
shadowing, as it were, the beautiful inflexions of the dentine and
cementum of the same part in the tooth of ZT. communis. The apex
of the pulp-cavity rises into the crown; it is filled with a brittle cone
of spar ; and the base of the cavity contains a small plug of osteo-
dentine, the vascular canals of which inosculate through the open
end of the cavity with those of the external sheath of cement, just
as In I. communis.
In the spinal column 56 vertebre, connected in an unbroken
series, now occupy 8 feet; but the hinder ones have slipped slightly
——
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1871.] HULKE—KIMMERIDGE ICHTHYOSAURUS. 441
on one another. The first forty-five bear a double costal tubercle,
and the remaining centra have a single one. The fifth, sixth, and
seventh centra are each ‘8 inch long; the fifteenth is rather less
than -9 inch. The vertical and transverse horizontal diameter
cannot be accurately taken. The length of the hindermost centra
is rather under ‘8 inch, while their transverse horizontal diameter
exceeds that of any of the preceding ones. The ribs do not offer
any thing peculiar; towards their vertebral end they are compressed
and channelled; in the flank they have a cylindrical form ; and their
ventral ends are flattened.
A pair of flat bones going below the early thoracic ribs are, I
infer, from their position, and from their close association with the
scapule, the coracoids. Their form is unusual. They are much
more elongated in the direction of the trunk’s axis than are those
of the Liassic Ichthyosawrt with which I have had an opportunity of
comparing them, their axial diameter being to their transverse one
as 5:3: 2°8 inches. With this greater length their anterior border
reaches much further forwards in advance of the glenoid cavity than
in the Liassic forms; and it, as also the median border, is straight,
so that the latter touches its fellow throughout its whole length
when the two coracoids remain naturally united, as they do in this
instance. The articular end of the scapula is unusually broad.
The paddles, particularly the hind ones, are extremely reduced.
Their precise form and composition cannot be learned; for most of
the lesser bones are missing. The humerus is 2:7 inches long, its
distal end is 2-1 inches broad, and the diameter of its middle is 1-6
inch. The femur is only 2 inches long; its proximal end is 1:4 inch
broad, its distal end is 1-1 inch, and the diameter of the middle is
*9 inch.
This, as I believe, new species, which I propose to call TI. enthe-
kiodon, resembles in the slenderness of its snout the two Liassic
species I. longirostris and I. tenwirostris, but it is readily distinguish-
able from these by the following characters. Its snout, relatively to
the length of the cranium, is not so long as that of J. longirostris ; its
smaller tooth-root is smooth, and not distinctly fluted as in J. tenui-
rostris; the shape of its coracoid is quite different from that of
the coracoid of tenuirostris; and its spinal column is much stouter
than that of either of these species. It resembles both J. tenwrostris
and JI. longirostris in the preponderence of its fore paddles over its
hind ones; but its fore and hind paddles, so far as I can judge of
their size by that of their proximal bones, are very much smaller ;
indeed the paddles, relatively to the whole skeleton, are smaller
than in any other species known to me.
EXPLANATION OF PLATE XVII.
Skeleton of Ichthyosaurus enthekiodon from Kimmeridge Bay, one twelfth
natural size.
442 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 7,
3. Note on a Fraeuent of a Terzosavrian Snour from KimMERIpeE
Bay, Dorser. By J. W. Huxxs, Esq., F.R.S., F.G.S.
[Puate XVIIT.]
Tuts piece of a Teleosaurian snout, which fell last winter from the
cliff in Kimmeridge Bay, and was lately entrusted to me by J. C.
Mansel, Esq., F.G.S., seems to me worthy of a short notice, as it is
the first indication of this genus which, within Mr. Mansel’s know-
ledge, has been discovered at Kimmeridge ; and I do not find in the
British Museum any Teleosaurian fossils from this locality, nor are
any mentioned in Mr. Seeley’s recent catalogue of the fossil Reptilia
in the Woodwardian Museum, although in both these collections there
are Teleosaurian remains from other Kimmeridge-clay localities.
The fragment, 17 inches long, represents a very long and slender
snout tapering gradually and slightly (ats breadth decreases only
0:5 in. through a distance of 15:5 in.) to behind the external nos-
tril, where the premaxille suddenly and largely expand. The
nostril, wholly inclosed in these bones, is dilated, strictly terminal,
and directed obliquely forwards; its lower margin is interrupted by
a prominent median tubercle formed of the swollen preemaxillary
suture; and a shallow convex lobe projects from the middle of the
upper margin. The premaxille ascend 2°5 in. above the nostril,
and end in an acute point, the maxille composing all the remainder
of the fragment. The upper surface of the snout is convex trans-
versely, more so in front than posteriorly, where it becomes de-
pressed; but its transverse section nowhere approaches the semi-
circular form of the stouter-snouted Steneosaurus Manselii, which I
described last session. The lateral margins are slightly crenated by
the prominent alveoli of the sixteen foremost maxillary teeth, the
openings of which slant outwards and downwards, while the hinder
ones look directly downwards. The palatal surface between the
alveoli is convex transversely in front, and it becomes gradually
flatter posteriorly. Throughout its whole length it descends below
the level of the alveoli. No trace of the front ends of the palate-
bones are discernible. .
Most of the teeth have fallen out ; but a few, broken short off, re-
main in the sockets. The transverse section of the best-preserved of
these teeth, at the neck, is nearly circular. Each premaxilla contains
five alveoli; judged of by the size of these, the third and fourth teeth
were larger than the others, and the first and fifth were the smallest.
Each maxilla in the space of 15-5 in. has a series of twenty-five
alveoli, of which the three front ones are smaller than the others.
The dilatation of the terminal nostril is much greater than in any
other Téleosaurus known to me. I believe the fossil represents a
new species, and I propose for it the specific designation megarhinus.
EXPLANATION OF PLATE XVIIL
Fig. 1. Snout of Teleosaurus megarhinus from Kimmeridge, seen from beneath,
reduced.
2. The same, from above.
~3. The same, from the left side.
Quart Journ. Geol. Soc Vol XXVII.PLXVIIT.
Maclure aMacdonaldimp:
Ne SONORA P ALY AEE pa
J.W. Hulke,Del:
TELEOQSAURUS MEGARHINUS.
1871. ] HULKE—KIMMERIDGE TELEOSAURIAN. 443
Discussion.
Mr. Srerey thought it likely that Mr. Hulke would eventually be
led to reestablish his genus Hnthekiodon. He remarked on the
peculiar characters presented by the specimen, and referred especially
to the coracoids, which were unlike those of Ichthyosaurus, but pre-
sented a close resemblance to those of Plesiosaurus. He considered
that there were indications of its having been connected with a car-
tilaginous sternum. The scapula furnished an important difference
in its widening, which formed a distinct acromion process. Mr. Seeley
remarked that double-headed ribs similarly attached occur only in
animals with a four-chambered heart, and that, considering this and
other characters, there was no reason for placing Jchthyosaurus lower
than among the highest Saurians*. He considered that the Teleo-
saurian snout differed from all known types.
Dr. Macponatp believed that what is called the coracoid has
nothing to do with the shoulder-girdle, and thought it might be a
part of the palate.
Mr. Manset stated, in answer to the President, that the fossils
were obtained from about the middle of the Kimmeridge Clay.
Mr. Erneringr suggested that it would be desirable to ascertain
whether the horizon of the Jchthyosaurus described was the same as
that of the specimens from Ely.
Mr. Gwyn JerrrEys inquired as to the food and habits of the
Ichthyosaurus.
Mr. Hvtxes, in reply, stated that, from the presence of a stain and
of numerous small scales under the ribs, the food of the Jchthyo-
saurus probably consisted of Squids and small fishes. He showed
that the so-called coracoid was clearly a part of the shoulder-girdle.
June 21, 1871.
Robert John Watson, Esq., B.A., Assistant Master at Dulwich
College; W. T. Scarth, Esq., Raby Castle, near Darlington; Gen.
A.C. Bentinck, of East Court, Wokingham, and John Brooke, Esq.,
of the Collegiate School, Newark, were elected Fellows of the
Society.
The following communications were read :—
1. On some supposED VEGETABLE Fosstts. By Witiiam CaRRuTHErs.
[Puate XIX.]
Tur baneful influence of the imagination in science is seldom more
clearly seen than in the way in which fossil botany has been too
often pursued. The determination of the name of a recognizable
* Having since seen the specimen, Mr. Seeley believes that the truncated
margin was anterior, and abutted against the interclavicle (episternum) ; so that
the posterior margins of these coracoid bones are similar to the same margins
in Ichthyosaurus, and there is no evidence of the animal having had a sternum.
444 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 21,
fragment can of course be made by any one who can intelligently
compare a specimen with a drawing or a description ; but the inter-
pretation of the affinities of a fossil or the restoration of a plant from
the few fragments known, can be accomplished only by one who has
some acquaintance with living organisms, and with the essential and
non-essential characters which combine or separate them. When
this knowledge is wanting, a lively imagination supplies its place
to the complete satisfaction of the investigator, but to the great
injury of science. From its very nature, moreover, an imaginative
interpretation is more tenaciously adhered to by its author than if
it were the legitimate deduction from known facts; and it is more
satisfactory, because it does not present the difficulties that are
always encountered in real life. It is quite in keeping with this
that a considerable contributor to the subject of fossil-botany has
declared that a knowledge of recent plants is a serious hindrance to
the investigation of fossil vegetables—and that another has recently
expounded in a science-lecture his important determination of the
affinities of Lepidodendron and Calamites to Lycopodium and Equi-
setum, although his descriptions make it evident that he never has
examined, and probably never has seen a single specimen of either a
club-moss or a mare’s-tail in his hfe.
I propose in this paper to call attention to some of the specimens
which I have either met with in collections, or have had sent to me
as fossil plants, but which have no connexion with the vegetable
kingdom. Instead of setting them aside as non-vegetable, I have
taken advantage of the opportunities afforded by my connexion with
the British Museum, and especially of the important assistance of
my friend Mr. Thomas Davies, to determine what they are.
It would be curious to trace such errors in scientific works, and
show how frequently careful observers have thought that they had
the most perfect foliage in dendritic crystals, and beautiful wood-
structure in stalagmites. But I have encountered errors more
remarkable than these, now happily exploded. Among others I may
mention :—a curious form of calamite from a particular bed in the
South Wales coal-field which turned out to be the fragment of the
handle of a Wedgewood basalt tea-pot ; a branching part of the root
of a great tree, the remainder of which was yet in sttwu and could be
obtained, converted into metallic lead; and a fragment of exogenous
wood showing the openings of the medullary rays, which was a sin-
gularly altered piece of shale or slate from the wall of a vitrified
fort.
The first specimen to which I would ask special attention is a
supposed fruit figured and described by Sternberg in his ‘ Flora der
Vorwelt,’ tab. ix. fig. 2, as Carpolites umbonatus. These are round,
flattened bodies, with a glazy polished surface and a central nucleus
(Pl. XIX. figs. 12-17); they sometimes separate from the matrix
enveloping them, and then appear to be fruits, with their pericarp
converted into a thin shining layer of coal, like the Trigonocarpons
that are found in similar beds. On careful examination, however, it
is seen that the glazy surface is not produced by a foreign substance,
1871.] CARRULHERS—SUPPOSED VEGETABLE FOSSILS. 445
but is the material of the bed polished in some way—and, further,
that the detached fruit-like body has many layers of such glazed
surfaces, subparallel to each other, and all separated by the ordinary
substance of the bed, which thus makes up the body of the so-called
fruit. The glazed lamine originate from the somewhat granular
nucleus. There frequently occur on the same hand-specimen small
patches of similarly glazed surfaces with irregular outlines (Pl. XIX.
tig. 12), to which the name Slickenside has been incorrectly applied ;
this term is properly employed and should be restricted to designate
the smooth and polished appearance produced by enormous friction
on the contiguous surfaces of a fault. The structures, however, in
shale, to which the name is applied are confined to the stratum in
which they occur, and never pass from one surface to the other;
they occupy all positions in the bed, and are isolated or sometimes
united at angles more or less acute; the polished surfaces are fre-
quently crumpled and waved. All these points in their structure
show that they are not due to a force external to the bed, and that
the polishing has not been produced by the sliding backwards and
forwards of the one surface on the other. Dr. Fleming carefully
investigated these appearances, and proposed what appears to be a
very satisfactory explanation of their origin. He believed them to
have been produced in cavities in a comparatively soft plastic matter
by the presence of water or gas contained in the cavities, and that the
specular aspect was the casting or impression of the fluid substance*.
These limited slickensides, or as I would prefer to call them fluid-casts,
occur in rocks which have been at one time or other in a more or
less viscous or tenacious condition; they are found in argillaceous
rocks of all ages. So also are the fruit-like bodies which I have
described; I have obtained them from the shale-beds of the Coal-
measures in England, Wales, Scotland, and North America, and from
the Newer Tertiary clays of Ulm, Wiirttemberg; they have been
figured from the Coal-measures of Germany, and from the Permian
rocks of Saxony. The granular nucleus which is found in the ceatre
of these fruit-like bodies, was, I believe, the source of the gaseous
substance which has left its impress on the glazed surface. This
nucleus appears to me to have been a crystalline concretion, which
subsequently decomposed ; and the gas then given off spread outwards
as it was produced in the planes of stratification, this being the
direction of least resistance.
These fluid-casts were figured by Rhode in his ‘ Beitrige zur
Pflanzenkunde der Vorwelt’ (1820) pls. vi., vil., ix., and x. The
first two plates give a faithful representation of the objects; but a
little play is given to the imagination in plate ix. ; and its unfettered
operation is seen in the tenth plate, where the different polished sur-
faces are converted into the petals of flowers, and the whole are
associated with foliage for which a species of Veronica has apparently
supplied the design.
The two following species have been based on these fluid-casts :—
* “Dr, Fleming on the structural characters of Rocks,” Proc. Roy. Soc. Hdin.
yol. ii, p. 170.
446 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 21,
1. Carporrres umBonatus, Sternb. Flora d. Vorwelt: Tent. p. xh,
tab. ix. fig. 2.
Cardiocarpum umbonatum, Bronn, Leth. Geogn. vol. i. p. 37, tab.
vii. fig. 3.
Guilielmites umbonatus, Gein. Leitpflanzen d. perm. Form. p. 19.
Quercites paleococcus, Unger, fide specimen in the Bruckmann
collection, British Museum.
2. GUILIELMITES PERMIANUS, Gein. Die Leitpflanzen der permischen
Formation, p. 19, tab. ii. fig. 6-9.
Carpolithes permianus, Schimper, Traité Pal. Vég. vol. il. p. 226.
Geinitz established the genus G'uclielmites for the reception of
these supposed fruits, because of their resemblance to the fruit of
Guilielma speciosa, Martius, a palm from Brazil. Schimper places
Guilielmites permianus among the fruits which he considers to be
related to the seeds of Cycadew ; while G. wmbonatus is not noticed
by him; it may be either rejected as a spurious fossil, uninten-
tionally overlooked, or referred to a place in the vegetable kingdom
which his valuable work has not yet overtaken.
There occur not unfrequently in the Stonesfield slate roundish
flattened bodies (Pl. XIX. figs. 4-7), most frequently exhibiting only
the amorphous cast of the organism in which they were originally
moulded, and lying loose in the cavity of the matrix, but occasionally
inclosed in a dark-coloured polished covering. These have been con-
sidered to be fruits; and they so closely resemble the aspect of the
ripe seed of a chestnut that it is not to be wondered that they are
always placed amongst vegetable fossils in museums. Some time ago
the Rey. P. B. Brodie, F.G.8., was so good as to send me his large col-
lection of Stonesfield-slate remains for investigation. I have already
described from them an interesting Araucarian cone. There were in
his collection several specimens of these round bodies, one with the
dark covering entire, and another with it partially removed. Besides
these I have examined a large series in the Oxford Museum, and
several in the British Museum. The continuous nature of the cover-
ing, without any indications of a base or apex, which would have
been indicated had it been a fruit, or of the hilum, had it been a
seed, made me doubt its vegetable nature ; and the uniform thickness
and continuity of the covering suggested that these bodies might be
eggs. Fortunately the surface yet exhibited sufficient markings to
assist in determining whether this was the case or not. After the
examination of a considerable series of eggs in the zoological collec-
tions of the Museum, I discovered that the sculpturing on the sur-
face agreed very closely with that on the eggs of reptiles, and espe-
cially those of turtles. This determination was confirmed when I
subsequently ascertained that the bony plates of Chelonians were
not uncommon in the Stonesfield slate. Besides turtles, however,
there occur also in this deposit the remains of Pterodactyles ; and it
is not improbable that they may be, as suggested by Mr. Seeley, the
1871.] CARRUTHERS—SUPPOSED VEGETABLE FOSSILS. 447
eges of these flying lizards (‘ Ornithosauria,’ p. 106). That they are
reptilian eggs there cannot be any doubt; and as they add somewhat
to the knowledge of the Reptilia of the Secondary rocks, and are
likely to be quoted by writers, I venture to give them a specific
name.
Mr. Buckman has already, in the Quarterly Journal of this So-
ciety, described some eggs which he discovered in the Great Oolite
of Cirencester. From their form he determined them to be reptilian ;
_and on examining the sculpturing on the surface of the egg, I find
his determination is confirmed. He proposed for them the generic
name Oolithes; and, employing this, I now add to the oblong form
described by him the round Sténesfield eggs as a second species, with
the designation Oolithes sphericus.
The Rev. Thomas Fox, of Brixton, Isle of Wight, has supplied
me with another and much smaller egg, which he obtained from the
Wealden in that locality, and which he also believed to be a fruit.
The three species may be thus characterized :—
Ooxrrnxs, Buckman, Quart. Journ. Geol. Soe. vol. xv. pa lO7,
O. satHonIcz, Buckman, Quart. Journ. Geol. Soc. vol. xvi. p. 107.
(Pl. XTX. figs. 8 & 11.)
Eggs ovate, twice as long as broad.
Locality. Great Oolite of Cirencester.
O. spH=RIcUS, sp.nov. (Pl. XIX. figs. 4-7, 10.)
Eggs globular, about three quarters of an inch in diameter.
Locality. Stonesfield Slate, Stonesfield.
O. oprusatus, sp. nov. (Pl. XIX. figs. 1-3.)
Egg small, subglobular, obtuse on one side, about three eighths of
an inch in diameter.
Locality. Wealden of Brixton, Isle of Wight.
Count Sternberg, in his great work on fossil plants, describes a
supposed Alga from Solenhofen under the name of Cystosedrites
nutans (‘Flora der Vorwelt,’ fasc. v. & vi. p. 35, 1833), having a
frond with linear branches bearing opposite, linear-lanceolate, a-
cuminate, faleate, and spreading leaves with a single midrib; and
the figure (7. c. pl. viii. fig. 1) agrees with the description, and with-
out doubt accurately represents the specimen. It has been since
ascertained that the drawing was made from an imperfect specimen
of a cuttle-fish, in which the body is wanting and the fleshy arms
have perished, leaving only their horny hooks somewhat in the posi-
tion they occupied in the animal. These Sternberg mistook for the
opposite leaves of an Alga. Munster figured a more perfect speci-
men, and gave to it the name of Acanthoteuthis speciosa (Beitrige,
fase. i. p. 105, pl. ix. 1843).
Among the specimens for the examination of which I am indebted
to the Rey. P. B. Brodie there is a delicate cuttle-bone, which so
closely resembles a leaf that it is not to be wondered that it was
448 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 21,
placed among the vegetable fossils. It belongs to the genus Teu-
dopsis, Deslongchamps, which is distinguished from Loligo only by
the different form of its horny pen. In the recent genus the pen 1s
lanceolate, with a long and slender shaft in front, while in Teu-
dopsis it is spatuliform, with a short and somewhat broad shaft in
front. Specimens found at Calvados show the ink-bag still pre-
served and in its proper position.
To this I propose to give the name of Teudopsis
Brodiei. This interesting fossil was obtained by the
Rey. P. B. Brodie from the insect-bed of the Purbeck
series of Dorsetshire, in which he has done such
important service to geology by his patient and
persevering investigation of the fragmentary remains
of insects buried in it.
The species hitherto known are all from the
Upper Lias of France or Wirttemberg ; this species,
therefore, carries the form somewhat higher in the
geological series. The following diagnosis will be
sufficient to distinguish it :—
Trupopsis BRopIEzI, sp. nov.
The horny bone anteriorly elongated and tapering
to the (broadish) apex. The boundary lines of the
anterior portion subconcave, extending two-thirds
down the bone, where it reaches its greatest width ;
the posterior portion oval, with a blunt termination.
The whole surface is marked by faint longitudinal
strie, which diverge outwards on the expanded
portion of the bone.
Teudopsis Brodiet.
EXPLANATION OF PLATE XIX.
Figs. 1-3. Oolithes obtusatus, Carr.
Figs. 1 & 2, natural size. The ruptured opening, through which the clay
filling the interior obtained access to it, is shown in fig. 2. Fig. 3.
Fragment of the shell, magnified, to show the markings on the surface.
Figs. 4-7, 10. Oolithes sphericus, Carr.
Fig. 4. Specimen in which the amorphous material filling the cavity of
the egg remains. Figs. 5, 6. Two views of the same egg nearly covered
with its shell. Fig. 7. The internal cast of another, showing, around
the edge where it is still inclosed in the matrix, portions of the shell
still remaining. These figures are the size of nature. Fig. 10. Frag-
; ment of the shell, magnified, to show the markings on the surface.
Figs. 8, 11. Oolithes bathonice, Buckman.
Fig. 8. Natural size. Fig. 11. Fragment of the cast of the shell, showing
the markings of the surface.
Fig. 9. Fragment of the shell of a recent Turtle.
Figs. 12-17. Fluid-casts in shale from Carboniferous rocks.
Fig. 12. Exhibiting three small fruit-like casts, and a flat irregular-shaped
cast. From South Wales. Figs. 15, 15. Specimens from Cape Breton,
N. America. Figs. 14, 17. Specimens from South Wales. Fig. 16.
Specimen from Old Cumnock, Ayrshire. All natural size.
OSI ake
; |
Quart. Journ.Geol Soe Val
Se ee ee
a
a
W.G.Smith, FL.S. fee. W.West &C° my.
Supposed Vegetabie Fossils.
1871.] GREEN—DONEGAL. 449
Discussion.
Mr. Srriry remarked, as to the compressed spheroids found in so
many rocks, that there was a difficulty in accepting the view of
their originating in fluid vesicles, though he was unable to suggest
any other theory by which to account for them. He observed that
the eggs from the Stonesfield Slate closely resemble those of some
birds in the pitting of the egg-shell, which differed from the pitting
on such reptile-eggs as he had examined—and that it was of the
highest interest to find such eggs in strata containing so many re-
mains of ornithosaurian forms, such as Rhamphorhynchus and Ptero-
dactylus, of which latter genus these were probably the eggs.
Prof. Rurzrr Jonzs fully recognized the ingenious explanation
of the bubble-formed limited slickensides that looked so much like
possible fossil fruits, and Mr. Carruthers’s masterly treatment of the
other specimens; but he wished that the author would take up the
subject exhaustively, and define the nature of other supposed vege-
table fossils, such as the so-called fucoids, Palwochorda, Paleophyton,
Oldhamia, &c., many, if not all, of which Prof. Jones thought to be
due to galleries and other tracks made by Crustaceans.
Prof. Ramsay had known many instances of such blunders as
those pointed out, made, not by experienced geologists, but by
those unacquainted with the science. Though he had never regarded
. the flattened spheroids as fossils, he was unable to account for their
_ presence in the clay-beds of different ages.
Mr. Hvrxe inquired whether Mr. Carruthers regarded the limited
slickensides common in the Kimmeridge shales as due to gaseous
origin. He remarked on the rarity of Pterodactylian remains as
compared with those of other Saurians in the Wealden beds, in
which the presumed eggs of Pterodactyle were found.
Mr. Suetey did not regard the Wealden egg as that of a Ptero-
dactyle.
Mr. CarrurHers, in reply, remarked that the local slickensides
mentioned by Mr. Hulke differed in character from those to which
he had referred.
2. Norss on the Grotoay of part of the County of DonEGAt.
By A. H. Green, Esq., F.G.S.
[ Abstract. |
- In this paper the author described the geological structure ‘of the
country in the neighbourhood of the Errigal Mountain, with the
view of demonstrating the occurrence in this district of an inter-
stratification with mica-schist of beds of rock which can hardly be
distinguished from granite, the very gradual passage from alterna-
tions of granitic gneiss and mica-schist into granite alone, and the
marked traces of bedding and other signs of stratification that appear
in the granite, to which the author ascribed a metamorphic origin.
He also noticed the marks of ice-action observed by him in this region,
and referred especially to some remarkable fluted bosses of quartzite,
and to the formation of some small lakes by the scooping action of ice.
VOL. XXVII.—PART I. : 21
450 PROCEEDINGS OF THE GEOLOGICAL socrETy. [June 21,
Discussion.
Mr. Forzes stated that none of the facts of this communication
were new; but he dissented altogether from the conclusions arrived
at by the author in regarding these rocks as originally of sedi-
mentary origin, and for the following reasons:—(1) That this dis-
trict had been studied in detail by Mr. Scott and Prof. Haughton,
who declare the rock to be undoubtedly intrusive, as it not only.
sends out veins into the neighbouring strata, but also encloses frag-
ments of the rocks through which it has broken. (2) Because the
author starts from the idea that if such rocks are found to lie con-
formably on beds of undoubted sedimentary origin, it is a proof of
their being themselves sedimentary or stratified,—a conclusion which
is totally unwarranted, since there are innumerable instances, not only
of beds of lava or other igneous rocks being conformable to fossili-
ferous strata, but of their also being found intercalated with such
beds even for considerable distances. (3) The strata, so far from
being proved by him to be of truly sedimentary origin, are of a most
questionable origin, since they are neither in themselves fossiliferous,
nor can they be correlated with any containing fossils as proofs of true
sedimentary deposition ; and the description of his section is sufficient
to show this; for although it looks well on paper on a scale of 3 feet
to the mile, the author has so little confidence in it that he is not
even certain as to which is the top or bottom of the section on
which so much generalization is based. (4) That a parallel struc- -
ture equally, if not better, developed than any occurring in the
gneiss of Donegal is common to many volcanic rocks, as in a speci-
men laid before the meeting, in which this parallel foliated structure
due to crystallization-layers is so well developed as to make it appear
exactly like a stratified rock, and even split along these lines ; and
this, although the product of volcanoes still active, is found for
great distances both overlying conformably and intercalated be-
tween beds of the Cretaceous and Oolite formations.
Mr. Scorr was unwilling to accept the section given by the author
as satisfactory, but stated that Mr. Green had, without knowing of
the existence of his papers on Donegal, confirmed many of his obser-
vations. He agreed with him as to the bedded appearance of the
granite, and to the masses lying in general conformably with the
lines of stratification of the country. The nearest spot at which
fossiliferous rocks occurred was separated from the beds described
by the whole width of the county of Tyrone, though some presumed
Eozoonal forms had been found at a less distance. He was not pre-
pared to believe in the original absolutely fused condition of granite,
nor in there being two distinet types of granite, one metamorphic
and the other purely igneous.
1871. ] LOGIN—NORTH-INDIAN GEOLOGICAL CHANGES. 451
3. Memoranpa on the most recent Grotocicat Cuanczs of the Rivers
and Puatns of NortHern Inpra, founded on accurate SURVEYS
and the ARTESIAN WELL-BORING at UMBALLA, to show the practical
application of Mr. Loctn’s THrory of the abrading and trans-
porting power of water to effect such changes. By T. Loetn, Ksq.,
F.R.S.E.
(Communicated by Alfred Tylor, Hsq., F.G.S.)
[The publication of this paper is deferred. ]
(Abstract. )
Tuer author commenced by referring to the general conditions of
the surface of the country under consideration, and to the evidence
afforded by it of a great decrease in the amount of rainfall, and a
great change in the nature of the rivers. His object was to show
that the superficial deposits of the plains of India were formed by
the action of mountain-streams, the deposits being irregular trans-
versely, but exhibiting a uniform section longitudinally, in a curve
which the author believed to be a true parabola, as indicated by
Mr. Tylor. The connexion of this with the author’s theory as to
the transporting power of water was indicated. The author also
showed that the beds of the large Indian rivers are rising rather
than being lowered, and pointed out that this was in accordance
with his theory.
iS)
=
N
PROCEEDINGS
OF
THE GEOLOGICAL SOCIETY.
POSTPONED PAPERS.
1. On the SrructurE of the Crac-Beps of Surrotk and Norroix,
with some OBSERVATIONS on their ORGANTc Remains. By Josupy
Prusrwicn, Esq., F.R.S., &e., President. Part [11.—Tue Nor-
wico Crag anp WestLeron Beps.
(Read January 26, 1870*.)
[Puate XX.]
In the first and second parts of this paper+ I described the
structure of the Coralline and Red Crags, and discussed the con-
ditions under which they were formed. It now remains to describe
the structure of the Crag series in Norfolk, and determime the
correlation of the two geographical series.
The order of succession in the Suffolk area is clear and defined ;
but the relation which the Crag-beds of that area bear to those of
the same series in Norfolk does not admit of the same ready deter-
mination. The Norfolk beds themselves, in their several localities,
have been described by Mr. R. C. Taylor +, Mr. 8S. Woodward §, Mr.
Charlesworth ||, Sir Charles Lyell §[, and Mr. Trimmer ** ; and more
recently a good brief account of them has been given by the Rey.
J. Gunnyy; whilst various papers, by Mr. Searles Wood $$, Mr. S
* For the discussion on this paper see Quart. Journ. Geol. Soc. vol. xxvi. p. 282.
t Anté pp. 115 & 325.
t “On the Crag-strata at Bramerton,”’ Trans. Geol. Soc. 2nd series, vol. i.
p- p. 371, 1826.
§ Outlines of the Geology of Norfolk, 1833.
i “On the Crag,” Lond. & Edinb. Phil. Mag. 1835-36; and Ann. Nat.
Hist. vol. ix.
q ‘‘ On the Relative Ages of the Crags of Norfolk and Suffolk,” Mag. Nat.
Hist. vol. iii. 1889; and “On the Tertiary Strata of Belgium &e., Quart.
Journ. Geol. Soc. vol. viii. p: 277.
** “On the Cliffs of Norfolk,” Quart. Journ. Geol. Soe. vol. i. p. 218, and
vol. vii. p. 19.
Tt Sketch of the Geology of Norfolk, 1864.
§§ “On the Extraneous Fossils of the Red Crag,” Quart. Journ. Geol. Soe.
yol. xy. p. 82; and “On the Structure of the Red Crag,” Quart. Journ. Geol.
Soe, vol. xxil. p. 538.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK, 453
Wood, jun. *, Mr. J. E. Taylor +, Mr. Harmer +, and Mr. Maw §, the
Rey. O. Fisher ||, Mr. Ray Lankester 4], and others, have since con-
tributed largely to our knowledge of it. With respect to these papers,
many of which (those especially of Mr. Wood and his colleagues)
are marked by much research and original opinions, I feel rather
at a loss how to proceed. Were I to give the views of each
author and discuss the points of difference between us, I fear I
should have to lengthen this paper to an extent which might be
wearisome to the Society. If I do not therefore always notice all
the points wherein I may agree or differ from other observers, I
beg they will not consider it arises from oversight, or from want of
due estimation of their researches, but from the mere necessity of
avoiding the long details which a discussion of the controverted points
would entail. I may be further justified in this course by the cir-
cumstance that my own researches are in great part anterior to
most of the papers in question. It may be observed that where
the several conclusions arrived at thus independently prove to be
concordant, they must be entitled to greater weight. One object of
this paper is also to give more fully than has been hitherto done
the stratigraphical details of the several pits and particular coast-
sections in which the relation of the several beds can be determined,
following their range from the Red-Crag district and proceeding
northwards through the Norwich-Crag district.
I described the Chillesford beds in 1849; and I then expressed
an opinion that they were probably of the age of the Mammali-
ferous Crag of Norfolk, or possibly one degree more recent, an
opinion shared by Mr. Searles Wood after an examination of the
fossils **. My own observations, continued since that period, and
the active researches of many of the geologists just named, have
confirmed that suggestion. It has further been shown that the
Norwich Crag may be divided into an upper and lower division,
the former corresponding with the Chillesford Sands and possessing
a deeper-water fauna of a more northern character than the other,—
conclusions which I accept with, possibly, a few modifications.
Another interesting question raised by Mr. 8. Wood, jun., and his
colleagues relates to the position of the Weybourne Crag; and on
this we do not altogether agree.
In my last paper it was shown :—that the Chillesford Clay was
probably the upper and deeper-sea portion of the second or higher
* «On the Red and Fluvio-marine Crags” &c., Ann. & Mag. Nat. Hist. March
1864; ‘On the Upper Tertiaries of the Hastern Counties, 1865; Geol. Mag.
vol. v. p. 452; Quart. Journ. Geol. Soc. vol. xxii. p. 546.
+ Geol. Mag. vol. iii. p. 273, vol. iv. p. 331, and vol. vi. p. 231. __
t Ibid. vol. vi. p. 231. § Lbid. vol. iv. p. 560.
| “On the Relation of the Norwich Crag to the Chillesford Clay,” Quart,
Journ. Geol. Soe. vol. xxii. p. 19.
@ Quart. Journ. Geol. Soc. vol. xxi. p. 221; and Geol. Mag. vol. iv. p. 91.
vol. v. p. 254, and vol. vi. p. 47.
** Instead, however, of their overlying both the Red and Coralline Crag un-
eonformably, I afterwards found that, while they were unconformable to the
latter, they succeeded to and passed transgressively off the former.
454 : PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
division of the Red Crag; that the Chillesford series filled up and
levelled the irregular surface of the Red and Coralline Crags, over
the highest portion of both of which it extends; that reefs of the
Coralline Crag divided the Red-Crag sea into different areas, with
local variations in the distribution of the Molluscan fauna; and
that the area north of Aldborough was not only separated from
the more open sea to the south, but was also more subject to the
influence of fresh water, the beds at once being more littoral and
containing a larger number of freshwater Testacea. The Chillesford
Clay was traced to Southwold, where it holds the same relation to
the shelly sand-beds as it does in the Chillesford and Sudbourne
districts.
Beyond the few pits in the neighbourhood of Southwold and
Wangford there are no sections of the crag in north Suffolk. On
the borders of Norfolk, however, we reach a section of great interest,
which was discovered a few years since by Mr. Rose, of Yarmouth.
It is in a brick-pit in the parish of Aldeby, at a distance, by road,
of four miles from Beccles.
The section is as under :—
Fig. 27.—Pit at Aldeby.
feet.
@. Valley-oravel v.20... acnsescc<sossnenss«derceccsartsctavesdedsnn. soesees ease 2 to 4
SH Chillestor@iclay (icc ede tccsesnesteawels soda de cbs daeelentactttabttdeceblestee aes eee 5 to r
3’. Light-coloured sands, with seams of fine gravel and of shells............
A boring has been carried through sands 10 feet deeper, when the tool was
stopped by a bed of gravel.
The Chillesford Clay is well developed, with its usual chanaeteis
of a laminated grey micaceous clay ; but no shells have been found
in it here. Large flints, little worn, and fragments of wood are
occasionally met with ; and Mr. Dowson informs me that he found
in the upper part of the clay the condyle of the femur of Elephant.
The marked feature of the section is the occurrence of the Crag
shells, not, as usual, with the larger portion in a comminuted state,
but entire and with a number of double shells, many in the same
position as when living. Occasionally large masses of flint are found
in the sand. I saw one which weighed 3 cwt.; and adhering to it were
numerous basal plates of the Balanus porcatus. The undisturbed
condition of the beds offers an unusvally favourable opportunity of
investigating the fauna of this part of the series free from the intro-
duction of any foreign element,—an opportunity of which Mr. W. M.
Crowfoot, and Mr. E. T. Dowson, of Beccles, have taken excellent
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 455
advantage. The collections of these gentlemen now contain above
seventy species from this bed; and [am indebted to them for the
following list * :—
Last of Shells found at Aldeby by Mr. W. M. Crowfoot and
Mr. EH. T. Dowson.
c. common. r. rare. fr. fragments. ve. very common. vr. very rare.
ne. notcommon. For one or two specimens numerals are given.
Bivalves. Pecten tigrimus ...............+6- ne
(Mbtatalban issiciecvodbectcscesss vr Opercularis! s.css-.ss<s+-ees 00 ne
[PIISIEMERINE?), ~ GAcoobadacosssocas r Pectunculus glycymeris?, worn 1
Anomia aculeata ......2.......-.-+ r Saxicava rugosa and var. ...... c
—— ephippium ...............- a Solen siliqua ?, fragment......... vr
Shilabaeceeeesccecse pbeooseedeo r Tellina fabula ....... goscabooossesn 1
Astarte borealis ............---s0 Yr ————Wleitieli, souscakneasntcessoenacce as ve
compressa, 2 vars. ......... ve —— obliqua............. sSbosboesto ve
SU Callas. cesaceaseenemelngsesece ve preetenuis ........ gadadboodd c
Cardrom-edulle.......-J0-c.n-00ne c Thracia phaseolina ............... ne
grenlandicum ........ secon Wot all) GRITS IGVENE Weecancdodeadansecdedatos ve
——_ TOOSUM ..........secereveeee Yr
strigilliferum ? ............ vr :
@bchlodbamna complanatum ... Yr TEED Es:
Corbula striata...........-.ssceceee ve | Acton tornatilis................0. r
Cryptodon sinuosum ............ vr | Bulla regulbiensis ............... vr
Cultellus pellucidus............... r —— truncata .........cc0......005 vr
Cyprina islandica ............... ve | Calyptrea chinensis ............ r
MowaxiyilttatUss.scee.ceas cece es c Capulus ungaricus, var. ...... 1
Kellia ambigua .........s00-20005 i Cerithium tricinctum ............ 1
Theda limatuila) 3...22226ces.acc0aces ec Chemnitzia —?, fragment ...... 1
pygmea (Bell) .......00008 1 Clavatula linearis................5. vr
Lepton nitidum ...........<...--- r TURTLE I EY Ae oanbaqaber seeesoder c
Loripes divaricatus .......... Seaoo We || Lely Guna) oven wiles 1 caaeAboedodoacooos vr
Lucina borealis ............2.006 - ve | Littorina littorea.................. r
Lucinopsis undata ........00+006 vr | Natica clausa ...........-.00.0.00 ve
Mactra ovalis ............ sppnoceac ve Ihelicoides: 7-5 ¢t.2.---20asees r
Solidar cscevescecs Ae tees r Purpura laps eeeecseseseesaecee r
subtruncata.......0.. paaec80s vr Ringicula buccinea ............... vr
Modiola modiolus ............... vr VEMbILCOSalaeenccehee se eenee vr
Montacuta bidentata ............ 1 Scalaria greenlandica ............ r
FELLUSINOSA .....0.c0...0c000- r iMrevelyanayccscscceercsesc he r
substriata...... conpeootens6n0c vr | Trochus tumidus........ Serer ror ce
Mya arenaria <.......0.eeeeee000es ve | Trophon antiquum ............... ip
truncata .........0. sonnoonse r Turritella communis ............ vr
iMiyinluisteduilisy cesceseesc-a ce ae
Nucula Cobboldiz ............... c Balanus crenatus .............0.008
tenuis ..... Seances ponesos Saco | ae POLCATUS anc cree dee seste coe
As the pit is a small one, and the sands are only occasionally
excavated, it is easy to see how rich and promising the locality is.
In the shell-bed a few Mammalian remains have been found, in-
cluding tooth and part of antler of Deer, teeth and bones of small
Rodent, vertebre of Whale, together with bones and vertebre of
Fish, otolites, spines of Echini, Foraminifera and Bryozoa.
There are no Crag-pits between Aldeby and the neighbourhood
of Norwich, where we have the well-known sections of Thorpe,
* Jn this list, as well as in that of Mr. Reeve, the greater part of the species
have been, I understand, determined by Mr. Searles Wood.
456 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Postwick, and Bramerton, each pit presenting certain distinctive
paleontological characters. In future collections from these beds it
would be very desirable to keep the fossils of each pit and each bed
separate, as has been so well done by Mr. Reeve for Bramerton.
The pit near the Asylum at Thorpe exhibits the best-known
and most interesting section of the Norwich Crag. Mr. R. Fitch,
F.G.S., of Norwich, has made a very fine eollection from this pit,
including a large series of Mammalian and Mollusean remains. The
former, which are common chiefly amongst or immediately upon
the basement bed of worn flints (#’, fig. 28), consist of teeth and
bones of the following species * :—
Mastodon arvernensis. Trogontherium Cuvieri.
Hlephas meridionalis. Arvicola.
Ursus. fn
Equus plicidens ? pone: ebbinds: ;
Bos. Platax Woodwardii.
Felis pardoides. Raia antiqua. :
Hyena antiqua. Vertebree and otolites of fishes.
Cervus Falconer. Teeth of Shark.
ardeus. Crab (claws of, notch in edge as in
Lutra. Carcinus).
The shells are found in a bed of white sand with seams of small
flint-shingle, lying immediately over the basement-flints. ‘The more
common shells are, Tellina obliqua, T. lata, T. preetenuis, Mytilus
edulis, Lucina borealis, Cardiwm edule, Mactra subtruncata, Mya
arenaria, Buccinum undatum, Purpura ltapillus, Natica eatena?,
Cerithium tricinctum, Littorina littorea, and L. rudis. Many species
are very rare ; and doubt attaches to some unique specimens in the
older collections. Mr. Fitch’s collection, which contains a typical
and distinct one from the Norwich district, eonsists of about 72
species of marine shells. They are ineluded in the lst of the Nor-
wich-Crag Testacea appended to this paper, which is taken chiefly
from the list drawn out by the late Dr. Woodward for Mr. Gunn,
supplemented from my own and other collections.
Fig. 28.—Thorpe pit, Norwich.
E feet.
SSS SSS ee 5. Ochreous and ferruginous
SSS ——
= ———— sands and Amnthieantet with
— = a layer of iron-sandstone,
————— = | full of casts of shells at x... 20
= SSS > 3. Grey clay (Chillesford), with
SS == =| a few large worn flints ...1 to 12
SSS SSS = 3'&2’/. White sands, with seams
SS of gravel and patches of
3 === shells and comminuted
= ——— ae with a layer of large
See —— SRG nts at base ...... from 5 to 12
=X W''5ywy & — At this pit the line of separation be-
SS eee ez!) tween 3’ and 2’ is not well marked.
TIC NAS as Sw At Bramerton 3! & 2’ are much thicker
[3 STW ea, ON Sate eee Chalk. (nearly 30 feet), and the division into
separate beds more apparent.
* Tn the revision of the mammalian remains I haye been kindly aided by Mr.
Boyd Dawkins.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 457
This pit shows also the relation of the Crag-beds to the overlying
series. I give the section (fig. 28) I took in 1856, as at that time
a thin seam of clay, which is probably the equivalent of the Chil-
lesford Clay, and a layer of pebbly iron-sandstone, with casts and
impressions of shells, were well exposed at the east end of the pit*.
On that occasion also I found a fragment of Deer’s horn immediately
upon the Chillesford Clay in the ferruginous gravel.
Mr. R. Taylor, so early as 1826, ‘showed j in his section of Bra-
merton pit that the fossils were grouped differently in the several
beds, and that some of the shells were peculiar to certain beds.
Mr. J. E. Taylor has recently + shown the differences to be still
more marked. He found that the upper beds of the Norwich pits
were characterized more especially by the much greater abundance
of deeper-water and more northern shells, and the lower beds by
a more littoral and freshwater group. Mr. Taylor and Mr. S$.
Wood, jun., refer this upper division to the zone of the Chillesford
series. This, as they justly notice, is an important elimination,
as it places the lower division of the Norwich Crag on terms which
admit of a juster comparison with the Red Crag of Suffolk, to which
they refer the lower beds. On general grounds I had long held
these two crags to be synchronous; but the correlation of the
molluscan fauna still presented some difficulties, which this deter-
mination of Mr. Taylor may help toremove. Owing to the absence
of sections in Mr. Taylor’s paper, I am uncertain how far I agree
with him in correlating these divisions at Bramerton with others
at a distance from Norwich and on the coast. The Chillesford Clay
is not visible in the Bramerton pit; but I have found traces of it in
the road leading up the hill at the back of the pit.
I am indebted to Mr. James Reeve, Curator of the Norwich Mu-
seum, for the following carefully worked out list of the shells from
Bramerton, showing, I believe, more completely than has hitherto
been done, the species proper to the upper and lower divisions. For
a further list, comprising all the species recorded from the Norfolk
Crag, I beg to refer to the general list at the end of this paper,
where, in column VI. the different localities at which the several
species have been found are given :—
Inst of Shells in the Norwich Museum from the Sand-pit on the
Common at Bramerton, collected by Mr. Reeve.
Univalves. Upper Lower Univalves. Upper Lower
Beds. Beds. Beds. Beds.
Admete viridula ......... ...... 1 Clavatula turricula ...... ver Yr
Buccinum undatum...... c e Conovulus pyramidalis.. ...... ie
Bulla obtusa............... vr r Hydrobia ulvee............ .....- vr
Calyptreea chinensis ... ...... r Lacuna crassior ?......... «2... 1
Cerithium tricinctum... ¢ c Littorina littorea ......... ec ve
Chemunitzia internodula. ...... vr MEU GUISE ae piscemeonee rs mE mG
_ * On visiting this pit again last summer (1870) I found the same beds sul better
exposed at the west end of the pit. The clay there varies from 1 to 2 feet in
thickness, and the iron sandstone is about 1 foot thick. The former contains
some large subangular flints, but no shells; the latter is full of well-preserved
shells (see Geol. Mag. vol. vil. p. 939.)
t Geol. Mag. vol. iii. p. 273, vol. iv. p. 331.
458
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Last of Shells (continued).
Univalves. Upper Lower Bivalves. Upper Lower
Beds. Beds. Beds. Beds.
Nassa —?, 8. T. ....ce0e) coer x Diplodonta astartea...... t
incrassata............ vr r Leda lanceolata ......... ...... fr
propinqua ......... ...... 2 limatula ............ ce r
Natica catena ...........- ce ( epton nitiehum®) S....4) eee t
Clauisanieesesaee der | aaeeee vr Loripes divaricatus...... ...... r
erenlandica ...... ...... vr | Lucina borealis............ ne r
helicoides............ vr vr | Mactra ovalis ............ r vr
Odostomia conoidea...... ...... * SOlida ...........000 c ve
Patella vulgata............ .....- vr stultorum............ ses. r
Purpura lapillus ......... ce ve subtruncata......... c ve
Ringicula ventricosa ... vr Yr Mya arenaria ............ ec ve
Rissoa semicostata ...... ...... Yr truncata ..........6. seeeee ec
Scalaria greenlandica ... r ne | Mytilus edulis ............ ve ve
Trevelyana ......... .... .. vr | Nucula Cobboldiz ...... vr Yr
Tornatella tornatilis ... ...... r (RETAINS | $54 505d9e078000 vr vr
Trochus tumidus ......... r r Pectunculus glycymeris. ...... vr
Trophon antiquum ...... r c Pecten opercularis ...... r vr
scalariforme ...... ...... Tt Saxicava rugosa ......... r r
Turritella communis ne c Solen siliqua............... sce0es Yr
Incrassata ......... ne ec Tapes texturata ......... ...0 T
Velutina levigata......... ...... vr VWALYOWAEE) “acocagosenan coands tT
Buvaivest Tellina fabula ............ «2... t
Anomia ephippium ...... é r Sage JEN sadoanndedcosee 10 e ve
patelliformis ...... r ip obliqua............+.. ve ve
Astarte borealis ......... c r preetenuis............ c ve
compressa ......... ve i Thracia phaseolina ...... r vr
Cardium edule............ ve ve Trigonella plana ......... Va Ores
groenlandicum vr vr. || Venus fasciaita 27. s22cess. ences rr
Corbula striata............ ¢c r Brachiopod.
Cyprina islandica ...... e ve |! Rhynchonella psittacea.. ...... vr
Land and Freshwater Shells.
Bythinia tentaculata ... ...... vr | Cyclas cornea ............ ...0.. vr
Carychium minimum ... ...... t Pisidium amnicum ...... ...... vr
Helix hispida ............ css... Yr Foraminifera.
~~ pulchella ............ t Polystomella ............ ‘e e
Limniea peregra «0... sess. MET DinciRovaltarnt aur Hh Sok e e
FORINT Socnonsonacs doodes r series
Paludestrina subumbili- Fragments of Balanus are common
Cat We dccicrenenceasin sts vr ve | inbothbeds. Spines of Spatangus and
Paludina lenta............ ...... r small claws of Crab are scarce. Verte-
Planorbis complanatus.. ...... i bree and other small bones of fishes are
SJOWROTONS Goacccoodeoa dosnon vr | common in the lower bed and rare in
Pupa marginata ......... ...... T the upper one. Remains of Arvicola
Succinea putris ........5 ...... tT very rare in either. Remains of Ele-
Valvata cristata ......... 2... vr | phant and Mastodon have been quoted
piscinalis............ vr vr | from Bramerton, but they are very rare.
In addition to these, Mr. Harmer has found the Panopea norvegica and
Trochus zizyphinus in the lower bed, Astarte sulcata, Abra alba, and Nucula
nucleus in the upper bed.
Postwick pit has long been noted for the occurrence of Rhyncho-
nella psittacea and for the annelid-drilled surface of the chalk at the
base of the crag.
* From a bank im a lane leading to Bramerton.
+ These are from a small adjacent pit in Mr. Blake’s grounds, in which
Serobicularia piperata (Trigonella plana) occurs in abundance.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 459
At Coltishall, 8 miles N. of Norwich, the relation of the Crag to
the Chillesford Clay is again clearly shown in the pit at the lime-kiln
(fig. 29).
Fig. 29.—Chalk-pit, Coltishall.
fe
we 8. Boulder-clay (traces of).
‘ 5. Ochreous and ferrugi-
nous sand and shin-
2 (alk) e cesad aaron eroes 12 to 15
3. Grey clay, with a few
fragments of wood
and a seam of peb-
bles (Chillesford
(len) cobpboasedeenee 6 to 8
2', White sand and fine
gravel, with patches
of shells and large
flints at base (Nor-
et.
a wich Crag) ......... 4 to 6
The shells collected by Mr. Reeve* and by myself in bed 2’ are:—
Astarte borealis. Littorina littorea.
compressa. —— rudis.
Cardium edule. Purpura lapillus.
Corbula nucleus. Scalaria groenlandica.
Cyprina islandica, Turritella incrassata.
Mactra ? Natica catena.
Mya arenaria.
Mytilus edulis. Helix hispida.
Pecten opercularis. Limneea palustris.
Tellina obliqua. Planorbis complanatus.
—— preetenuis.
Teeth and bones of the Mastodon are occasionally found at the
base of the same bed. One of the workmen informed me that he
had also found bones above the clay (3).
In the closely adjacent pits at Horstead the Chillesford Clay may
be seen holding the same position. But in one pit (the old water-
channel) the sand bed (2’) under the clay is not fossiliferous,
whereas the one above it (5) is; whilst at the farmyard-pit, close
by, the lower bed (2’) is fossiliferous and 5 is not. An entire skele-
ton of Mastodon is said to have been discovered in 2' some years since.
Thence we pass to the coast at Cromer without meeting any
more Crag-pits t. At Cromer traces of the Crag were found lying
on the chalk in digging the foundations of the jetty ; but no section
of it is seen until we reach Runton Cliff.. At a short distance
west of the Gap a ferruginous pebbly mass of crag, 2 feet thick,
* In addition to these, Mr. Reeve has found in the same bed at Wroxham,
two and a half miles 8.8.E. of Coltishall pit, Nucula Cobboldie, N. tenuis, Leda
limatula, Lucina borealis, Mactra subtruncata, M. solida, Tellina lata, Anomia
ephippium, Trophon antiquum, and Pecten tigrinus, but no freshwater shells, no
Turritella, and no Astarte borealis.
t My friend the Rev. J. Gunn has this summer been with me to the pits
at Burgh, between Coltishall andWeybourne. The Chillesford Clay is again well
exposed there, and overlies a foot or two of pebbly sand, which contains in places
a few Norwich-Crag shells.
460 PROCEEDINGS OF THE GHOLOGICAL SOCIETY.
rises at the base of the cliff, and is overlain by 3 feet of laminated
clays with imperfect impressions of plants and traces of shells.
The crag may be traced more or less well at the base of the
cliff thence to Sherringham. Here it assumes larger proportions.
On one occasion (in 1856) I found several undeterminable bones
in the iron pan (crag) lying on the chalk, but no shells; forty
yards further west the crag becomes more sandy, and contains
shells. The following is a section taken at the base of this cliff :—
Fig. 30.—Lower part of Oliff west of Sherringham.
6. Boulder-clay (base of). fect.
5. White sand and flint-shingle, with a subordinate bed of laminated clay .
(x) and a few shells in lower bed (aa) ....s..sscesceeeneeecececeeeenees 12 to 14
3. Grey clay, with fragments of wood (Chillesford Olay) ............... 3to 4
2'. Tron sandstone (pan) with a few shells, overlain at x’ by 6 inches of
sand with numerous shells, including Telina balthica...... igosooocte Ito 14
The pebbly sands (5) continue more or less shelly all the way to
Weybourne; and in places near Weybourne the surface of the
chalk under the crag has been pierced by Annelids and by the
Pholas crispata, whilst pebbles of chalk bored by Sawicava rugosa
are met with in the overlying craggy beds. These lower beds, which
Mr. Jeffreys has examined with me, contain the following shells col-
lected on the occasion of several visits :—
Cardium edule. Pholas crispata.
—— greenlandicum ? Saxicava rugosa.
Cyprina islandica. Venus fasciata.
de Con TESS, Buccinum undatum.
Mya arenaria. : Helix hispida.
Leda lanceolata. Hittorina rudis.
Mactra subtruncata. Nati ne
Nucula Cobboldiz. uit MeUgoider:
Tellina balthica. Ehagpumn pulls,
lata. Balanus crenatus.
—— obliqua. Bones and vertebree of fish.
Above these shelly sands the bed of clay (3), which I would
refer to the Chillesford Clay, can be traced with few interruptions.
It is not fossiliferous. Sometimes (as just west of Sherringham) the
sand and shingle (5) have worn down and denuded this clay, and then
in its place we often find a reconstructed bed, consisting of a base
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 461
of sand, and iron-sand, with fragments of wood, and flint-pebbles,
together with clay-pebbles of the destroyed bed, which latter are
in places so numerous as almost to hide its reconstructed character.
Immediately over this clay-bed is another series of sands and
shingle “5, which are often fossiliferous ; and when the clay-
bed is wanting, it is difficult to draw a line of demarcation between
the two series, especially as the fossils themselves, with the ex-
ception chiefly that the Tellina balthica is far more abundant, do not
show any very marked difference. The shells I have found are :—
Cardium edule. Mytilus edulis,
Cyprina islandica.
Leda lanceolata. Purpura lapillus.
Mya arenaria. Littorina littorea,
Tellina balthica. rudis.
— obliqua.
These, however, are, I believe, far from representing the fauna of
this bed, which is undergoing, I understand, in the hands of the
Messrs. Searles Wood, a thorough examination. The importance
to be attached to these beds does not arise so much from their ex-
hibition here, as from the circumstance that they will serve to
determine the position and age of beds of sand and gravel, gene-
rally without fossils, which have a wide range in the south-east of
England, and the exact position of which it is important to know
in consequence of their bearing on many interesting problems con-
nected with the denudation of the country. These beds, which over-
lie the Chillesford Clay and the Forest-bed, and are succeeded by
the lower division of the Boulder-clay, I propose to designate the
“* Westleton Sands and Shingle.”
As, however, some uncertainty may be considered to attach to the
clay which we have referred in Norfolk to the Chillesford beds, on
account of the absence of fossils and the presence also of laminated
clays in the overlying beds, we prefer to commence our observations
in a district where both the Chillesford Clay and the Crag-sands are .
distinctly developed, and where the relation of the several groups
to one another is more clearly determined.
Tur WESTLETON SANDS AND SHINGLE.
Between Yoxford and Dunwich there rises, just above the village
of Westleton, a ridge of low hills largely excavated at that spot for
sand and gravel. Nowhere, except on the north-west of Henham
Park, are these shingle-beds so largely developed. They attain a
thickness of from 30 to 40 feet, and consist of a series of stratified
beds of well-rounded flint-pebbles imbedded in white sand, and with
two or three subordinate beds of light-coloured clay. They look
more like the pebble-beds of Blackheath than any other beds in the
eastern counties. Mixed with the flint-pebbles are a few small
pebbles of old rocks, with a considerable number of white quartz-
pebbles, the presence of which constitutes a distinctive feature of
these beds throughout their range. No fossils are found here, and
no other beds are exposed. Elsewhere this series is generally not
462 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
more than from 20 to 25 feet thick; and sands predominate, the
shingle being subordinate.
In the neighbourhood of Reydon, near Southwold, the same beds,
usually light-coloured, are seen underlying the Boulder-clay in some
of the clay-pits ; but they are better exposed in the pits along their
line of outcrop on the north side of the valley of the Blyth, nearer
Southwold. In a pit close on the north-east edge of Reydon marshes,
I found in these sands, last autumn, a seam of the same pebbly sand
concreted by oxide of iron. This seam was full of the casts and
impressions of Mytilus edulis in all stages of growth, and many of the
shells double. Southwold* stands on these beds ; and their relation
to the Boulder-clay and to the valley-beds was well exposed before
the removal of the brick-pit, just north of the town, further from
the shore. The section was as follows :—
Fig. 31.—WNorth end of Southwold Cliff (see also coast sect. Pl. XX.).
a. Brick-earth and gravel, with the remains of Elephas primigenius ...5 to 10
8. Boulder-clay (upper division) .............2-cceeceeneenecnceseneccenereencens 8 to 12
5. White and yellow sand and shingle, with a few ferruginous bands ...... 20
In the next cliff, at Easton Bavent, we find the same sand and
shingle, with seams of the ferruginous bed. In the latter, casts of
shells are numerous, but difficult of determination. I found
Cardium, Mytilus (edulis ?), Littorina, Natica,
and numbers of small Foraminifera.
The Chillesford Clay here rises from beneath these shingle-
beds (5); and under the clay is the well-known Southwold crag
(ante, fig. 26, p. 345). This section clearly shows not only the re-
lation of these divisions, but in the same cliff, a short distance further
north (fig. 32), may be seen the setting-in of the Forest-bed and its
relation to the same series.
Fig. 32.—Section near the north end of Easton-Bavent Cliff.
feet.
==== 5 5 White and yellowsand and shingle 5
== 4 4. Traces of wood and carbonaceous
matter.
=== 3 3. Laminated grey clay with double
shells in the position of life (Chil-
iesstorgel, (CHER) coe sgnscoboosoonsoac8ss- 6
* But for the existing sands and shingle of Southwold strand, I should have
preferred ‘“‘ Southwold” to ‘‘ Westleton” to designate these beds.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 463
In the next range of cliffs the further relation of the same beds to
the Elephant-bed of Norfolk is shown. The higher part of the cliff
at Kessingland is formed by the upper division of the Boulder-clay.
Beneath are beds of sand with subordinate seams of small flint-
gravel, which may be referred to the Boulder-clay series, though
the lower part may belong to the Westleton beds. Beneath these
sands, and just on the same level asin the cliffs at Cove and Easton
Bavent (two and four miles south), the Chillesford Clay crops out
and ranges to near Pakefield.
Fig. 33.—Chff between Kessingland and Pakefield, about one mile
north of the former place.
a. Loamy sand and gravel ......... 4to 6
8 8. Boulder-clay (upper division)
15
to 20
7 7. Light-coloured sands, with some
seams of fine gravel and a few
fragments of shells «........ 20 to 25
= 5&@409 & 4 (traces of). Flints and iron-
sand, with rootlets running
down into 3 ...............e000e- Oto 1
= 3 3. Greenish clay (Chillesford Clay) 5
The clay is here more compact, and in places contains a number
of worn fragments of flint. No shells are found in it*.
The Forest-bed, together with the associated freshwater bed, now
becomes sufficiently well marked, as the following section shows :—
Fig. 34.—Lower part of Cliff 14 mile south of Pakefield.
—a T~ 2 wm tro ye. et ~o7. Mise
SS SF IS Se OAS ae Se BS Be SGEoo
= a — = Boulder-
clay).
—— = —— = === = = = = —e: =
7. As in fig. 35. 4. Forest-bed, 0 to 6 feet.
5. Elephant-bed, 1 foot. 3. Chillesford Clay.
At this place a depression in the Chillesford Clay has been filled by
a local freshwater deposit (4) consisting of a dark carbonaceous and
* Mr. Crowfoot informs me that he found a deer’s bone in this clay.
464 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
laminated sandy clay, at the base of which freshwater shells are
found. The shells are only in occasional patches, and consist of
Unio pictorum, Cyclas cornea, and Bythinia tentaculata*,
As we approach Pakefield the bed of shingle, which rests on the
clay (3) becomes ferruginous, and contains pebbles of clay derived
from the Chillesford Clay. A considerable number of mammalian
remains (EHlephant?, Rhinoceros, Deer, Ox, and Horse, the same appa-
rently as in the Forest-bed of Norfolk) have been found in this bed.
Besides the common occurrence in this cliff of rootlets passing
from the base of the shingle into the underlying clay to a depth of 4
or 5 feet, the trunk of a tree, 20 feet long, was found some years
since on the surface of the clay-bed (3), and nearer to Pakefield the
stool of a large tree was found in stu, as at Hasborough.
Nearer to Pakefield the Chillesford Clay is entirely broken up, and
a bed composed of sand, flint-pebbles, and pebbles of Chillesford clay
ae its place, while the « Westleton sand and shingle” is imme-
diately overlain by the upper division of the Boulder-clay.
At Corton, to the north of Lowestoft, the Forest-bed appears again
for a short distance at the foot of the cliff, with the Lower Boulder-clay
immediately above it, whilst the Westleton beds are wanting. They
arelargely developed inland, however, and are worked on the west side
of the Somerleyton brick-pit, and at several pits N.W. of Lowestoft.
From the cliffs at Corton, where we lose the Forest-bed, to the
cliffs at Hasborough, where it again crops out at the foot of the cliff,
is a distance of 24 miles. The Crag-beds beneath it there (if they
exist) are not exposed ; but in the series above it we find the same
order of succession as at Southwold and Kessingland. The Forest-bed
along this coast appears to exist, as between Pakefield and Kes-_
singland, under two forms :—-the one a local freshwater deposit of
grey and carbonaceous clay, contaming the remains of mammalia,
insects, plants, and freshwater shells; and the other of trees, rooted
sometimes in this bed and sometimes in the Chillesford Clay beneath
it. It is not often the latter is seen. It appears, however, on
the shore at low tide at Pauling. The Forest-bed itself has been
bored into at Hasborough by Mr. Gunn to the depth of 14 feet,
without reaching its base. From this point to Trimlingham none
of the beds under this level are visible; but the Westleton beds are
well exhibited at various places, as, for example, at the cliff north
of Bacton Gap (fig. 85; sce also coast-section, Pl. XX.).
Fig. 35.—Oliff near Bacton.
6. Boulder-clay (lower division) with
fragments of shells.
5. Sandy flint-shingle with seams of
laminated clay (@) and fragments
of wood ; shells at places in lower
part of the shingle, 10 to 12 feet.
5’. Elephant-bed............ 3 to | foot.
5, 4 Top of Forest-bed.
* Mr. Crowfoot’s Collection.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 465
The Westleton beds here exhibit the characters we have noticed
further south, consisting essentially of flint-pebbles with numerous
white quartz-pebbles and a small admixture of pebbles of some pecu-
liar varieties of siliceous sandstone, chert, and slate rocks; mixed
with them is a considerable quantity of drift-wood, both in large
pieces and in matted small branches. Further, the basement bed
of this series again often contains at places clay-pebbles derived
from the Chillesford Clay *.
At this part of the coast the Westleton beds become more argil-
laceous, containing several subordinate beds of laminated grey
clays without fossils. These clays sometimes replace, in great part,
the sands and shingle, whence Mr. Gunn has applied to this series
on the Norfolk coast the term of “the laminated clays,” which
often well expresses their charactery. In this area the Westleton
beds rarely exceed 25 feet in thickness; and where the Forest-bed
rises higher, as at Paston Cliff (fig. 36), or where the underlying beds
have been denuded before the deposition of the Boulder-clay, they
are sometimes wanting.
Fig. 36.—Section in Paston Chiff.
7. Sands, gravels, and laminated loams (base of 7).
6. Boulder-clay (lower division).
5. Sandy shingle.
5’. Elephant-bed.
4, Forest-bed.
As we proceed further northwards these beds assume a fluvio-
marine character. Just south of Mundesley a thin seam of clay with
freshwater shells, consisting of
Anodonta cygnea, Pisidium amnicum,
Unio pictorum, Bythinia tentaculata,
Sphzerium corneum, Valvata piscinalis,
which I have already described t, appears at their base; whilst on
the north of Mundesley marine shells are intercalated with seams
* T had not found any shells on this part of the coast; but Mr. Gunn pointed
out to me this summer.a spot about half a mile north of Bacton Gap, where we
procured from the lower bed of the Westleton shingle the following shells :—
Purpura lapillus, Littorina rudis and L. littorea, Mytilus edulis, and a species of
Scalaria, allmuch decayed. Some years since, Mr. Green, of Bacton, stated that
the Crag was found in Bacton cliff; but his statement remained discredited.
This was no doubt the bed to which he referred.
+ I hesitate to adopt this term, as the character is again repeated in the beds
above the Lower Boulder-clay in the same cliffs, as well as in the Chillesford
beds below. Nor in any case is a mineral designation convenient, especially for
such variable beds. (See also my paper on the Mundesley Section, in the
* Geologist’ for 1861, p. 68.) ¢ ‘The Geologist’ for 1861, p. 68. .
VOL. XXVII,—PART I, 2k
466 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
of freshwater shells throughout the series‘. It is the ferruginous
“pan” lying at the base of this series, which is so rich in mam-
malian remains, and is known as the Elephant-bed. It is, however,
clear that the Westleton beds often repose upon a much denuded
surface of the underlying beds, the débris of which they then
contain. Therefore how far the bones found in the Elephant-bed
may be proper to it, or how many have been derived from the
Forest-bed, is uncertain, as it has not always been possible to keep
the fossils of the two beds distinct, nor is it always practicable to
distinguish the proper from the extraneous fossils +.
A large number of these mammalian remains were collected by
Miss Gurney ; and Mr. Gunn’s magnificent collection, which he has
also lately presented to the Norwich Museum, is known to all
geologists. Dr. Falconer, who studied them with so much zeal, has
left a number of interesting notices respecting the more important
specimens, in those memoirs in which he investigates the characters
of the Proboscidia §.
Mr. Gunn, in his excellent concise account of the Forest-bed, in
which he includes the Elephant-bed as an upper division, gives the
following list of mammalian remains ||, chiefly on the authority of Dr.
Falconer, to which Mr. Boyd Dawkins has obligingly added the
species marked with an asterisk.
Elephas antiquus. Cervus megaceros.
—— ——, var. priscus. —— elaphus.
meridionalis. Sedgwickii.
Rhinoceros megarhinus. —— Poligniacus.
—-—— etruscus. capreolus ?
Hippopotamus major.
Equus («caballus).
Machairodus?
Bison priscus ?
Bos (*primigenius).
Sus (xarvernensis).
Ursus arvernensis.
* speleeus ?
* etruscus ?
*¥—— ardeus.
Trogontherium Cuvieri.
Mygale moschata.
Sorex fodiens.
remifer.
Arvicola amphibia.
Castor europzeus.
Two species of whale.
[ Vertebrz of fish. |
+ Mr. Gunn has also pointed out to me a spot, just under Mundesley, where
a pebble bed, with Littorina, Mytilus, &e., just as at Bacton, occurs, and a little
to the north the Pinna pectinata is found.
+ A large proportion of the fossils have been collected from the shore after
storms, when they had been washed out of the cliffs ; and many have been dredged
out at sea. Those which are derived from the elephant-bed frequently have a
portion of the gravel cemented to them, which may show that they are not derived
(directly, at all events) from the forest-bed; but I would observe that the
“pan” at the base of the Crag, and immediately lying on the Chalk, presents
lithological characters not to be distinguished in detached portions from the
other; and as I have found bones in this crag-bed at Sherringham, this bed
may, although not so rich as at Norwich, have supplied a portion of the re-
mains found on the shore.
§ ‘Paleontological Memoirs and Notes,’ edited by Charles Murchison, M.D.,
1868, vol. ii.
|| Mr. Gunn considers that there is evidence of several] other species of Deer,
and two more varieties of Elephant, in the Forest-bed.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 467
Sir Charles Lyell, in his ‘ Antiquity of Man,’ gives a list of the
plants from the Forest-bed, determined by Dr. Heer, they are :—
Pinus sylvestris. Nuphar lutea.
Abies excelsa, Ceratophyllum demersum.
Taxus baccata. Potamogeton.
Prunus spinosa. Alnus.
Menyanthes trifoliata. Quercus.
Nympheea alba.
. To these Mr. Gunn adds rhizomes and fronds of Ferns.
The insects have not yet been fully described. They include
several species of Donacia.
The following affords a good general section of this series, lying
beneath the Boulder-clay, in this part of the coast.
Fig. 37.—Section of the Westleton Beds near Mundesley.
a. Laminated grey clay without fossils.
——a
The total
6. Sand aud small gravel with freshwater shells.
c. Laminated grey clay.
marine shells: oblique lamination common.
d. Sand and gravel with fragments of wood and |
e. Fine sand.
= f. Clay and gravel with M/ytii and Limnee.
g. Laminated grey clay.
a eel h. Coarse gravel. Elephant-bed.
SSS Dark sandy clay. Forest-bed.
These beds vary too rapidly to give
their relative thickness.
thickness may be taken at 25 feet.
4
These beds may be followed, with few interruptions, to Trimling-
ham and Cromer. Mr. Gunn states that it is from these beds at
Bacton that the remains of two Whales were obtained; and it is
probable that, as the Forest-bed is not exposed at Cromer, the Nar-
whal tusk and the remains of a Walrus found by Mr. King near
Cromer were also from the sand-and-shingle beds.
The next point of interest is near Runton Gap, where we again
find at the base of the series a bed of peaty clay full of the following
species of freshwater shells :—Bythinia tentaculata, Valvata piscr-
nalis, V. spirorbis, Planorbis marginatus, P. fontanus, Limnea pa-
lustris, Paludina achatina, Pisidium amnicum, P. nitidum, Spherium
corneum, Anodonta cygnea, Unio pictorum, U. margaritifer. Some
years ago Mr. Trimmer discovered in the sand and shingle between
this peaty bed and the Lower Boulder-clay, at Runton Gap, a bed
containing numerous Mya truncata and Leda myalis in their natural
vertical position, with both valves perfect. The section is as shown
in fig. 38.
This brings us back to the part of the cliffs deseribed (ante, p. 460)
in the section on the Norwich Crag. The beds now ae ae subordi-
re
468 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
nate fluviatile seams, and, in proceeding westward, instead of an
occasional seam of Mytili or My or afew Lnttorme, we get fossili-
ferous beds so like the Norwich Crag that they were always referred
Fig. 38.—Section of the Westleton Beds on the side of Runton Gap.
feet. feet.
a, Valley-gravel.
6. Boulder-clay ...........ssssseesercnceecees 8 to 10
5. Beds of light-coloured sand and flint-
shingle, with shells at x, and a
freshwater peaty bed at X X_ ...... 12 to 15
to that series. But Mr. Searles Wood, jun., on paleontological evi-
dence, places them on a higher zone. The difference between Mr.
Wood and myself is, that I think the lowest beds “ 2'” from Runton
to Weybourne should be referred to the true Norwich Crag, whilst I
would refer the upper shell-beds ‘‘5” to the Westleton series, in-
stead of putting them all together, as I believe Mr. Wood does, into
one zone, higher than either of these*. At this part of their range
there is, with the exception of the presence of the more numer-
ous fossils, little difference in their character from that of the same
beds in the neighbourhood of Southwold, where the fossils are
rare and, with few exceptions, in the state of casts and impressions
onlyt.
Taking a line from Weybourne to Norwich, the Westleton beds are
scantily exhibited over the Chillesford Clay at Burgh and Oxmead.
At Coltishall they are more fully developed and contain a subordinate
bed of iron-sandstone and clay-ochre, 14 ft. thick, which reposes
upon a slightly denuded surface of the Chillesford Clay. At Horstead
the Westleton shingle with crag-shells overlies the Chillesford Clay
(ante, p. 459). This is the shelly bed to which Mr. 8. Wood, jun., has
applied the name of “ Bure-Valley Crag.” It is seen again at
Belaught, and still better at Wroxham. At the latter place there
are two pits, in one of which a thin bed of Norwich crag, with
numerous single valves of the Cyprina islandica, overlies the Chalk,
and underlies a thin bed of clay, representing, probably, the Chilles-
ford Clay, and in the other the same clay is overlain by a sandy crag
characterized by the presence of numerous Tellina balthica.
I have already (ante, p. 456) shown the relation of the typical
* Quart. Journ. Geol. Soc. vol. xxii. pp. 547-549. The only other alternative
that I could admit is, that they all belong to the Westleton series.
t I have one perfect valve of Tellina balthica from near Pakefield.
{ Freshwater shells again appear in these beds. I found, this autumn, in a pit
near the Anchor Inn, Coltishall, Limnea palustris associated with Tellina bal-
thica, Mya arenaria, Cardium edule, Littorina littorea, and Cyprina islandica.
PRESTWICH—CRAG=BEDS OF SUFFOLK AND NORFOLK. 469
Norwich Crag to the Westleton beds at the Thorpe pit. The latter
there put on the character of a coarse ferruginous shingle passing
under the Boulder-clay series higher up the hill; but that is not
seen in this pit. The shells of this ferruginous bed (#5) consist, as
far as they have been determined by Mr. Reeve, of :—
Cardium edule. Modiola (large sp.).
Mytilus edulis. Littorina littorea.
Mya arenaria. Purpura lapillus,
Tellina obliqua.
There is, however, nearer Norwich, a section which, although
wanting in the confirmation afforded by organic remains, shows in a
very interesting manner the superposition of the whole series, and
the relation of different members of the Crag and glacial beds in this
district (fig. 39).
Fig. 39.—Pit at Bishopford Bridge, Norwich.
ly stratified flint-gravel ......
(=?)
GUN MSO) sco cacqonasccooadonooussan .
ou
5. White sands and flint-shingle
(Westleton beds) .........2+0...
3. An irregular seam of grey clay
VO) 3'(?) & 2’. White and ochreous
sands, and flint-shingle and
gravel. Small patches of shells
(Norwich Crag) found occa-
sionally in the lower part, and
Chalk. large flints at the base .........
Nie
ee Oe ee FL
\
|
feet
7 7%. Coarse ochreous loamy rough-
25
6. Brown Boulder-clay (lower
15
20
(Chillesford Clay?) ......... Otol
470 PROCEEDINGS OF THE GEOLOGICAL SOCIETY,
Conclusion.
Nothing can be clearer than the relation of the Red to the Coral-
line Crag; but the Norwich Crag occupying a different area, and each
area presenting a crag-series of its own type, without superposition
or passage, their relation to one another must necessarily be esta-
blished on other grounds. We have to see what other beds there
may be common to the two districts, whether in each they bear
a like relation to those Crag beds which are the object of inquiry,
and whether the differences known to exist in the latter may not be
owing to geographical distribution. :
Tn this case we have the one common bed in the Chillesford Clay,
which forms a zone limiting in ascending order the position both of
the Red and of the Norwich Crags, both of which it overlies and
with both of which it shows a close relation. But although we can
follow the Chillesford Clay (retaining its usual characters and fossils)
into the southern part of the Norwich-Crag area at Southwold, north
of that district it is not fossiliferous and we can only identify it by
position and mineral characters. Nevertheless we can follow this
argillaceous zone, although a character of uncertain value, with
sufficient clearness to Bacton and Weybourne, and also inland to
Norwich and Coltishall. In Norfolk, however, as the sands and
shingle overlying the Chillesford Clay become interstratified with
beds of laminated clay very similar in appearance to the Chillesford
Clay, it might be a question whether the bed which I have referred
to that deposit in Norfolk belongs to it, or whether the Chillesford
Clay is represented by the Laminated Clays of Mr.Gunn. Mr. Gunn
contends that such isthe case. Although I am ready to admit that,
on lithological characters alone, the evidence would be almost as good
for one as for the other, still I think that the clear superposition of
the Chillesford Clay to the Crag, and its infraposition to the West-
leton shingle, at Easton Bavent, with the commencing indications of
the Forest-bed at the same place, and its clearer exhibition at Kes-
singland, accompanied by the setting in, in the same cliff, of the
Elephant-bed—taken in conjunction with the presence of the Mas-
todon in the Norwich Crag and its absence in the Forest-bed, and the
difference in the species of Elephant, Rhinoceros, Deer, d&c. in the two
series—sufficiently prove their relative position and age. Mr. Gunn’s
Laminated Clays constitute a subordinate lithological character of
the Westleton series in Norfolk, and are occasionally present in
Suffolk.
The Forest-bed, of which we get indications at Easton Bavent, is
more fully developed at Kessingland and Corton, at which latter
place it passes under the lower division of the Boulder-clay, the
Westleton shingle having been denuded as it occasionally has been
even in the Hasborough and Mundesley district (see fig. 36, p. 465).
At Hasborough and Bacton the base of the Westleton shingle
is usually cemented into a hard “pan” by oxide of iron, and
constitutes the well-known Elephant-bed. ‘This reposes upon the
¥orest-bed, which, in its turn, rests on the Chillesford Clay when
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 471
that is not denuded. Between Hasborough and Sherringham, the
latter usually lies at too low a level to be exposed. When it does
appear, the relations to the Norwich Crag and to the Westleton
beds remain constant, in the same way as at Coltishall, Wroxham,
and Thorpe.
I have, in my last paper, noticed that the rich fossiliferous beds of
the Red Crag of Walton, Sutton, and Butley become poorer after
passing beyond that area, that at Chillesford the number of species
is much less, and that the same poverty characterizes the few pits
on the west flank of the Coralline ridge of Sudbourne.
North of this ridge the Crag at Aldborough is still poorer; but still
the fossils are all Red-Crag species. At Thorpe the facies of the
fauna seems different; but this is chiefly due to the difference in the
relative proportion of the species. There is not a single new species
of Mollusca; but such species as are found on the beach of a sandy
bay abound. The Littorina littorea, scarce at Chillesford, Butley,
and Aldborough, is here abundant, as are also the Mya arenaria,
Mactra ovalis, and Cardium edule, whilst Natica, Cerithiwm, and
Turritella become much more common. At the same time some
fragmentary mammalian remains, vertebre and teeth of fish, and
fragments of Crustacea are also more numerous. At Sizewell the
Conovulus pyramidalis is a common shell. At Bulchamp and at
Easton Bavent freshwater shells increase in number, and the Corbi-
cula fluminalis* and the Astarte borealis make their first appearance.
But of 43 other species of marine shells I have collected at Thorpe,
Sizewell, Bulchamp, and the neighbourhood of Southwold, there is
not a single species which is not found also in the Red Crag. In
both also some species, such as the Tellina obliqua, T. lata, and
Purpura lapillus, continue to be very abundant, and the Cyprina
islandica is common. In lithological character the only difference is
the greater extent of gravelly (flint) beds and the absence of the
ferruginous colouring, though that exists at Sizewell and Bulchamp,
Neither of these characters is of any importance.
Probably Thorpe, Wangford, and Bulchamp (in part) may be re-
garded as the equivalents of the lower division of the Red Crag,
whilst Sizewell and Easton Bavent should be referred to the upper
division or Chillesford sands.
This upper division is better exposed at Aldeby, where a large
addition is made to the number of species ; several new forms appear,
while some old forms of the Red and Coralline Crags reappear.
In the neighbourhood’ of Norwich the Rhynchonella psittacea + comes
in, and on the coast at Sherringham the Tellina balthica is added to
the fauna. In the upper bed of the Norwich Crag at Bramerton and
Thorpe many of the species found in the lower bed are wanting, but,
with the exception of the accurate lists of fossils from the Bramerton
pits made by Mr. Reeve, we are yet without fully sufficient separate
lists of the two divisions of the Crag, whether in Norfolk or in
* Mr. Bell has lately found this shell in the Red Crag at Waldringfield.
+ Also lately found by Mr. Bell in the Red Crag at Shottisham.
472 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Suffolk, although we have good lists of special localities. That such
a division exists in Suffolk, both lithologically and paleeontologically,
there can be no doubt; and that it is to some extent maintained
in Norfolk is probable. But in Norfolk it is not always easy to
show the line of separation, and it becomes a question whether the
differences in the Molluscan fauna are not differences produced in
the fauna of one period by local conditions of sea-bed, depth, and
fresh waters. There is no doubt that the lower beds, both in Suf-
folk and Norfolk, are more-shallow-water deposits, and that, in the
latter county especially, they contain a large freshwater element ;
while the upper beds, with greater depth of water, show the Mol-
lusca less drifted, more in situ, and as having been under the influ-
ence of colder currents.
Not only, however, do the upper and lower beds differ, as at
Bramerton, but the same division shows marked differences in dif-
ferent pits. Thus the lower bed in the pit east of the one on the ~
common has been named by Mr. Reeve the Scrobicularia-bed, from
the abundance of that shell, of which only one or two fragments
have been found on the same level in the adjacent pit, while Zrophon
clathratus, Diplodonta astartea, and Tapes aureus have been found by
Mr. Reeve in the former pit and not in the pit on the common. So
Cardium edule and Littorina littorea are rare at Aldeby, but are very
common at Beccles (section of town well), while of the Cerithiwm
tricnctum, also common at Beccles, only one specimen has been
found at Aldeby. In the same way the fossils from the same beds
at Thorpe, Bramerton, Postwick, Coltishall, and Horstead present
marked differences of grouping and in relative numbers. So, as 1s
well known on our own coasts at present, the distribution of the
Mollusca presents rapid variation. Amongst other instances, Mr.
Jeffreys states that the Tellina balthica abounds in Swansea Bay,
but that not a single specimen is to be found at Oxwich Bay,
only nine miles distant. It is possible, therefore, that the differences
found to exist throughout the Norfolk and Suffolk areas are more
or less dependent on these causes—that Thorpe (Suffolk), Wangford,
Thorpe (Norwich), may represent old lines of coast or shingle-banks
in the old sea, while Sizewell, Southwold, Beccles, Aldeby, and
Bramerton may represent synchronous deeper-water deposits. Dif-
ference of depth is also probably the eause why the fauna of Aldeby
is so mueh richer than that of the upper division at Bramerton, and
why so many of the older Coralline-Crag species reappear. I have
therefore, for the present, taken the two divisions together; and this
gives the following result :—
Total number of species recorded in the Norwich Crag ............ 179
: Deduct land and freshwater species ............ccseeesseeenes 24
doubtful and varieties ...............:.ccsseeeneseesees 16
— 40
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 473
The relation which these species (155, including the varieties)
show to the Red and Coralline Crags of Suffolk is as follows :—
Bi- Uni-
valves. valves. Total.
Common to the Red Crag.............+. 69 ... 68 = 187 or 88 per cent.
Common to the Coralline Crag ...... 54 ... 83 = £87 or 56 i
We have before (ante, p. 352) seen that the number of species of
the Red Crag found in the Coralline Crag was 62 per cent.
With regard to the proportion, in the Norfolk-Crag period, of
existing species to those not known as living, the following is the
result, after excluding the 16 varieties and doubtful species :—
mos 5 Proportion of
Total. Living. Extinct, extinct species.
139 130 9 6°5 per cent.
Comparing the three Crags, the respective proportions of extinct
and living species of Mollusca in each is as under :—
Extinct. Living.
In the Norfolk Crag ....... ponsonos 6°5 93°5 per cent.
In the Red Crag of Suffolk......... 7 92:3 =,
In the Coralline Crag ............... 16:0 840 ~=CéS
showing so close a relation between the Norwich and Red Crags
as to afford good reason for considering them to be both of the same
age*,
With respect to the geographical range of the 216 living species
(exclusive of varieties and extraneous species) of the Red Crag, and
of the 130 species of the Norwich Crag, some marked differences
are noticeable, as shown in the following Table.
Table of Geographical Distribution of the Mollusca of the Red
and Norwich Crags.
Red Crag. Norwich Crag.
Ct C=
Bi- Uni- Bi- Uni-
valves. valves. Total valves. valves. Total.
ID CHIC Hee cacscascesteeces 21... 19 = 40 18... 18 = 36
North American...... Se MOR ash ee Mteteinti din) = ne
Scandinavian ......... 63) 22) = 185 42 ... 44 = 8&6
iBritishtasocsset daseakces bh = OOle = LST 42... 45 = 8&7
West European ...... 80°... 46> = 156 37... 86 = 73
Mediterranean ...... 79... 88 = 167 33... 34 = 67
Atlantic ............00 35 49 = 8&4 18 .. 20 = 38
Special localities.—Africa, 1; South Africa, 1; West Indies, 1 ;
Gulf of Mexico, 1; Japan, 3.
* Taking Aldeby to represent the upper division (or the Chillesford Sands)
and the lower beds at Bramerton the lower division (or the equivalent of the
Red Crag of Sutton, Waldringfield, &c.) of the Norwich Crag, we have the fol-
lowing results :—
Total Proportion of Numbers commen to the
= extinct to ——— See >
species. —_ living species. Red Crag. Coralline Crag.
per cent.
PANGODYN cr etsees ces: 71 56 53 38
Bramerton ......... 64 6 58 24
474 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
This gives a slight increase in the proportion of northern spe-
cies in the Norwich Crag, while the proportion of southern species
shows a greater decrease, but not more than might be dependent
on local coast conditions. The relative proportion of total British
species in the Red and Norwich Crags respectively is as close as
67:69, while the total northern forms show as 80: 105, and southern
forms 150: 104. Or, taking the species not now found living in the
British seas, their relative distribution in the three Crags is as
under :—
Species now restricted to
Total — — a~ —_———,
living species. Northern seas. Southern seas.
Norwich Crag ............... BION Seeeose dane: tS) eeBaesoodasc 11
Red Crag purity aes icine DAG) BSG ABE oror sa chente 32
Coralline Crag............... 7A 0) a RS ctr TA ries cue eee 65
So that while the relative number of British species, as well as of
the extinct species, remains nearly uniform, there is a considerable
decrease of southern and some increase of northern species in the
Norfolk area.
The relation of the two crags as shown by the Mammalian remains
is less conclusive ; but the differences are no greater than we might
expect from the evidently different relations of the land to the
water in the two areas. The same Mastodon*, Horse, Hyena,
and Felis occur in both; and there is strong reason to believe that
the Elephant (meridionalis ?) is likewise found in the Red Crag.
A Bear (arvernensis), and a Deer (megaceros), though not found in
the Norwich area, are found in the Suffolk Red Crag, and pass into
the Forest-bed, and must therefore have existed in the Norwich-
Crag period.
After carefully weighing all these considerations, I must confess
that, as I see no sufficient reason for regarding any of the Norwich-
Crag Mammalia as extraneous fossils, I now cannot but look upon
all species common to the two Crag areas, together with those species
which, though not found in both Crag areas, are still found in one,
and occur again in the later-deposited Forest-bed, as really con-
temporaueous fossils proper to the Red and Norwich-Crag series.
This view is in the main in accordance with that arrived at by Dr.
Falconer, upon the evidence of the contemporaneous continental
Pliocene fauna.
The Forest- and Elephant-bed inaugurate a condition of things
materially different from that prevailing during the Crag period. A
number of new Mammalia make their appearance, including the
Elephas antiquus and var. priscus in numbers, two new species of
Rhinoceros, a Hippopotamus, two Bears, together with species of
Horse and Ox, and some small rodents of existing species. But the
marked feature of the period consists in the number and variety of
the Deer, no fewer than six species, several of them of very peculiar
* As the occurrence of the nearly entire skeleton of the Mastodon at Horstead
shows that it lived in the Norfolk Crag area, I do not think that it can be looked -
upon as extraneous to the Red Crag.
PRESTW ICH—-CRAG-BEDS OF SUFFOLK AND NORFOLK. 475
types, having then flourished in considerable numbers. In the
Crag, all the Mammalia, except possibly the Arvicola, belong to
extinct species. In the Forest- and Elephant-bed, three species pass
in from the Crag, associated with thirteen other extinct species, and
with six living species of Mammalia. On the other hand, the shells,
whether freshwater or marine, so far as we can judge from the
limited number yet known, are of existing British species; and all
these, with possibly one or two exceptions, are species which are
continued up from the underlying Norwich Crag. The break in
time, therefore, between the Crag and the Westleton Sands and
Shingle is probably not inconsiderable.
These conclusions, whilst they agree in part with those of Prof.
E. Forbes, Sir Charles Lyell, Dr. Woodward, and Mr. Searles Wood,
with regard to the gradual lowering of the temperature from the
period of the Coralline Crag to that of the Forest-bed, differ from
previous results in the proportion of recent to extinct species, show-
ing a much closer approach to the existing fauna than before was
estimated to exist. In arriving at this conclusion I have had the
valuable assistance of Mr. Gwyn Jeffreys, whose researches in the
seas of Europe have done so much to make us acquainted with Crag-
species supposed to have been extinct, and with the variations pro-
duced by geographical distribution, nature of ground, and depth of
water. As an instance of the geological bearing of these consi-
derations, I will quote some remarks of Mr. Jeffreys * in speak-
ing of Mactra solida:—“I regard Mactra truncata as the littoral
or shallow-water and southern variety, and WM. elliptica as the
deeper-water and northern variety of one and the same species.” -
«« Every conceivable gradation of shape and solidity may be seen in
a recent state; and the union of WM. solida and M. ellipicca is cemented
by paleontological evidence.” “I may also observe that when M/.
solida gradually finds its way into deeper water than it had been
accustomed to, the shell becomes more slender and glossy although
nearly of the usual size. It has then all the appearance of MV. ellip-
tica.” He also alludes to the still greater difference in Buccinum
undatum taken at low water and at depths of from 70 to 80 fathoms,
as well as to the case of Venus gallina and other bivalves. It is
upon evidence such as this that Mr. Jeffreys has arrived at the con-
clusion that so many of the Coralline and Red-Crag species are to be
regarded merely as varieties.
In my former papers the conditions under which the Coralline and
Red Crags were formed, together with the mode of distribution and
relations of the fauna, were investigated. It was shown that at the
very commencement of the Crag-period a degree of cold prevailed
severe enough to give rise to the transport by ice into the Coralline-
Crag sea, not only of flints from the neighbouring chalk shores, but
* British Conchology, vol. ii. p. 418. This work is full of remarks interest-
ing to the geologist on the range and habits of most of our Pliocene and Post-
pliocene shells.
476 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
of boulders from a great distance, and that, during the formation of
the lower Coralline Crag, movements of subsidence prevailed, suc-
ceeded in the upper division by an elevation of the sea-bed, which
brought the Coralline Crag partly above the sea-level, where it be-
came exposed to the action of the tides, currents, and breakers of the
Red-Crag sea. In consequence of this action, a very large portion
of the Coralline Crag has been destroyed, and its débris incorporated
in the mass of the Red Crag; and the beds of phosphatic nodules
(or the Coprolite-beds) of the Red Crag are probably derived in whole
or in greater part from the Coralline Crag. Floes laden with large
unworn flints from the neighbouring chalk coast were stranded on
the Sutton Coralline-Crag islets, whilst shore-ice floating off from the
same islets strewed the sea-bed around them with large blocks and
boulders of the Coralline Crag.
The Norwich Crag, which occupies the contiguous area, and lies
on the same level, seems to have been divided from the more open
sea of the Red Crag by a barrier of Coralline Crag, behind which were
sandy bays, into which flowed a river or rivers bringing down land
and freshwater shells, and probably mammalian remains from land
to the north-west and west. There is evidence of these streams
coming from that direction in the circumstance that in the Crag at Nor-
wich, Lias Ammonites, Mountain-Limestone corals, besides the many
fossils from the Chalk, are found. I have found also, at the base of the
Crag at Weybourne, a fragment of fossiliferous Kimmeridge Clay,
and in the Norwich Crag an encrinital column similar to some I have
seen in the Red Crag of Suffolk, in which latter also occur Belem-
nites, Ammonites, Ostrew, and Terebratule from various Secondary
rocks, together with fragments of chert from the Lower Greensand,
while the occurrence of the fragments of red granite points to trans-
port from still more distant localities*.
After a time a general subsidence of the whole area took place,
followed by the deposit of the Chillesford sands over the irregular sur-
face of the Coralline Crag, Red Crag, and Norwich Crag, and at the
same time colder currents from the north introduced new and more
Arctic species of Mollusca. Still notwithstanding the greater depth
of water and the greater cold, there is an absence of all foreign
boulders, with the exception, if they may be so termed, of large blocks
of subangular chalk-fiints.
The sea-bed was then raised and a land surface formed in eastern
Norfolk, and over some adjacent part of the German Ocean. On
this freshwater deposits were formed, and a forest of Scotch firs,
Norway spruce and other trees of a temperate character grew.
The forest was frequented by herds of deer, whose shed antlers
are found in abundance (Woodward), as well as by troops of Hlephas
antiquus.
Another subsidence then took place submerging the whole forest,
* For considerations on the subject of the old Crag-area, and on the causes
modifying the Crag-fauna, see Godwin-Austen “ On the Kainozoic Formations of
Belgium” (Quart. Journ. Geol. Soc. vol. xxii. p. 228).
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 477
but still leaving land in the near vicinity. From this land wood
and freshwater testacea, and some mammalian remains were carried
down into the great beds of shingle forming off the coast in a sea in
which still lingered some of the Crag Mollusca. At the same time
a portion of the old forest land as well as of the marine clays
which preceded it were denuded. These sands and shingle are
of much greater extent than the forest-area, and spread over all East
Norfolk, Suffolk, Essex, and beyond. The main feature of this
deposit is the presence of flint pebbles with a considerable proportion
of white and pink quartz pebbles and a few pebbles of slate, toge-
ther with some rolled fragments of Greensand chert. On the table-
land above the Meuse, in Belgium, there is a gravel of a very similar
character ; and I think it not improbable that some old river tra-
versing the Ardennes may then have brought down into this Crag-
sea area the old slate, quartz, and quartzite pebbles found so abun-
dantly in the Westleton shingle, while other streams from the south
or south-west may have drifted in the chert from the Lower Green-
sand and the mass of flint pebbles from the Chalk *.
The relation of the Crag sea of Belgium with that of the south-
east of England has been the subject of frequent inquiry. Taking
the revised lists of M. Dewalque and those at the end of this paper,
the following results are arrived at respecting the species common
to the several deposits.
Numerical Distribution.
Total. | Sables gris. | Sables jaunes. | Sables noirs.
Norwich Crag ...... 155 60 68 ; 24
Suffolk or Red Crag| 273 122 138 61
Coralline Crag ...... 316 133 135 98
Proportional Distribution.
Sables jaunes. | Sables gris. Sables noirs.
Norwich Crag...... 43-9 38°7 15:5 per cent.
Suffolk or Red Crag 50:5 44-7 PES Slee
Coralline Crag ...... 42-7 42-4 SLOW. wes
This shows a more marked connexion between the upper or Red
and Norwich Crags and the Sables jaunes and gris, forming the Systéme
Scaldisien of Dumont, than was before noted; whilst the lower or
Coralline Crag seems to hold a place intermediate between these
beds and the Sables nozrs, or the Systéme Diestien of Dumont.
Such, then, are some of the changes which mark the epoch of the
* T have also met with rolled fragments of silicified wood, like that which I
have found i situ in the Woolwich and Reading Hocene series of Kent.
478 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Crag. Of the first great change produced by the emergence of land
to the south previous to the formation of the Red Crag we have
scanty evidence. Traces of a Crag of the age probably either of our
Coralline Crag or of the Crag noir exists in Touraine; so that until
that period there had been communication with southern seas and
an interchange of species*. The elevation of the Wealden dome
brought to the surface beds of early Crag or of Diestien age, portions
of which still exist in our North Downs at an elevation of from 500
to 600 feet? ; and a like elevated tract, capped by beds of the same age,
is prolonged into France and Belgium. This formed a barrier sepa-
rating the southern and northern sea areas, and so isolating the
fauna of the Coralline Crag, that, with the lower temperature of the
sea resulting from the exclusion of currents from the south and the
setting in of others from the north, a great part of that fauna died
out. It is a case of extinction by change of conditions, and not by
time.
This accounts for the disappearance in the Red Crag, noticed long
since by Mr. Searles Wood, of so large a number of the southern
genera of shells which characterize the Coralline Crag; while the
descent of the more northern genera continues, with little loss, ae-
companied by the introduction from time to time of new species of
northern forms.
A considerable number of the species which disappeared from our
area at the period of the Crag continued to exist further south in
the Atlantic and Mediterranean. Other species, under favourable
conditions of the low temperature at great depths, survived in the
mid-Atlantic, where their existence remained unknown until they
were recovered by the deep-sea dredging so successfully carried on
of late years. As many as 93 species of the Coralline Crag have
been found at greater or less depths in the southern seas ; and of
these, 17 met with at depths of from 1000 to 7000 feet had not
been before met with livingt. In the same way there are 65 species
of the Red and Norwich Crags row found ranging to great depths;
but of these, 39 lived at the time of the Coralline Crag; and of 4 of
these not before known, 2 are Coralline-Crag species.
'The presence of northern and arctic species does not, however,
necessitate a severe climate; for cold currents may give a northern
facies to the sea-fauna, while the land may retain the mean tempe-
rature due to geographical position. Beyond the introduction of
more northern forms of shells in the Red and Norwich Crags, there
is nothing to indicate a great increase of cold. None of the blocks
of the Coralline Crag have been found drifted far from the Sutton
islet. The porphyry boulder at the base of the Coralline Crag ex-
ceeds in dimensions any other foreign block either in the Red or the
Norwich Crag. In the Chillesford Clay itself nothing but large
* Only a few shells of the Faluns of Touraine passed into our Crag area; but
many of the Bryozoa are common to the Coralline Crag and Douay beds.
t Quart. Journ. Geol. Soc. vol. xiv. pp. 322 et segq.
t Quart. Journ, Geol. Soc. vol. xxvii. p. liy.
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK. 479
chalk-flints from neighbouring shores shows transport by ice. The
many fragments of secondary rocks and of mountain-limestone in
the Red and Norwich Crags were probably brought down by river-
action or river-ice. Nor is the increase in the northern species of
shells very great in ascending through the Norwich Crag, though
the number of individuals increases considerably, and a number of
southern species become extinct. At the same time it is singular
that so many Coralline-Crag species, mostly of British and Mediter-
ranean forms, should reappear in the last or uppermost stage of the
Crag at Aldeby.
This conclusion is in accordance with the land-fauna and flora we
find flourishing subsequent to the Norwich Crag. The winter cold
may have been greater; but otherwise the climate seems to have
been a moderately temperate one. In the Forest-bed the vegeta-
tion, whether as regards the species or the size of the trees, is far
from indicating a severe climate. Nor do we find any of the Mam-
malia which indicate extreme cold. The Mastodon no longer ap-
pears; but an Elephant, a Bear, and two Deer of the Crag period
survive. With these, however, some of the animals of the postglacial
period appear, showing probably the setting in of colder conditions
there or further north. In the Westleton shingle we get the drifted
remains of the same vegetation, and the same land and freshwater
shells ; but these latter are of a character common to all northern
and temperate Europe. ‘The marine Molluscan fauna now becomes
poorer, but still without any decidedly marked northern characters ;
nor are any foreign boulders found—nothing but drifted pebbles
carried possibly along a shore-line. Nevertheless we have in this
series the nearest known approach to the glacial period, which set
in immediately afterwards with a rigour and intensity denoting, I ap-
prehend, causes of an entirely different order from those, the effects
of which, up to this time, may be attributed to the known and
assignable influence of land configuration and oceanic currents.
480 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Lists of the Mollusca found i the Red and Norwich Crags.
This list is compiled like that of the Coraline Crag, with the excep-
tion of the Norwich-Crag species, which are largely supplemented from
the late Dr. Woodward’s list in the Rey. J. Gunn’s ‘ Geology of Nor-
folk,’ and from thelists furnished me by Mr. Reeve and Mr. Crowfoot
(see pp. 455 & 457). The new species introduced in the Red Crag by
Mr. Jeffreys, with the assistance of Mr. Bell, are marked J in column I.
The names to which at is prefixed denote species which Mr. Jeffreys
identifies with those now living, in addition to those recognized by
Mr. Wood. A form regarded by Mr. Jeffreys as a variety ranges
through all the columns in italics. In column III. are his critical
remarks, with the name first given to the species ; while other
names adopted by Nyst for the Belgian species are in brackets. The
names to which a { is prefixed denote recent or living species ; but
these species having been originally named from fossil specimens before
they were known as living, the original names are retained. The
species supposed to be derived from the Coralline Crag have Cor. Cr.
marked incolumn III. Column VI. gives the chief localities where
the species occurs in the Red and Norwich Crags. Column VII.
shows the species which occur in the Coralline Crag, column VIII.
those which occur in the Belgian Crags, and column IX. those which
are found at Monte Mario. For columns IV., V., and IX. I am
indebted to Mr. Jeffreys. The letter d prefixed to species in column
II. denotes those bivalves which Mr. Bell informs me he has found
perfect or having the valves united in the Red Crag (ante, pp. 330
& 351).
Localities in Red Crag:—A, Alderton; B, Bawdsey; Bw, Brightwell; Bt,
Butley; F, Felixstow; Fh, Foxhall; H, Hollesley ; R, Ramsholt; 8S, Sutton ;
W, Walton-on-the-Naze; Wd, Waldringfield.
Localities in Norwich Crag and Chillesford Sands:—Ad, Aldeby; Bl, Bul-
champ; Br, Bramerton; C, Chillesford; N, Norwich (pits not particularized) ;
P, Postwick ; E, Easton Bavent (Southwold) ; T, Thorpe (Norwich) ; Th, Thorpe
(near Aldborough) ; W, Weybourne Cliffs.
Geographical Distribution :—A, Arctic; Am, North American ; At, Atlantic ;
B, British; M, Mediterranean; S, Scandinavian ; W, West European.
Depth:—Lt, Littoral; L, Laminarian; C, Coralline; D, Deep-sea ; D,
depths exceeding 1200 feet.
Class I. BracuiopopA.
I. II. III. IV. V. Vir VII.j VIII.
Ke s Localities. ‘Beles :
“S| Names of Synonyms and Pons Geographical aD i | fs wi
° 5 Species. critical remarks. distribution. s ‘= op [= 8
2 8 depth. ‘Ss Es |ss
ad S 55 liso
a pS a ‘S)
16.|dTerebratula | Cor.Cr.(T.Sow-| ...... | ....s0e0 WdSR| ....... * fo? x
| _ grandis. erbyana).
21.)dRhynchonella| —.......0 L-D BSA NS) PT Br}...
psittacea,
ario,
_ Italy.
Monte Mi:
I Il. III.
°
man Names of Synonyms and
2 a Species. critical remarks.
&p ©
s 4
AY
237.| Abra alba ...... Genus Scrobicu-
laria.
238 fabalis ...\ S. alba, var. ...
240.| —— obovalis...| Hrycina ovata,
Philippi.
239. prismatica) _.........
9.| Anomia aculeata| A. ephippium,
var.
8. ephippi-| —.........
um, LZ,
10. patelliior=|" | 7 etccsea
wis.
$). striata ...| A. patelliformis,
var.
77.| Arca lactea...... eGiaie chasis
76.| —— tetragona | A. imbricata
215.) dArtemis lenti-| Venus exoleta,
formis. Linné,var.(Do-
sinia exoleta).
216.| d—— lincta......|G. Wenus (D.
lincta).
177.| dAstarte Baste-| A. sulcata, var.;
rotit. Cor. Cr.
175.] —— borealis...) .....eeee
188.| d-— Burtinii...| Cor. Cr.? ......
183.) d-— compressa| Not Venus com-
pressa, L.
184 crebrilirata| Crassina de-
pressa, Brown
190.) —— digitaria .| G. Woodia......
181 elliptica...| A. suleata, var.
185.| d— gracilis ...|A.compressa,var.
(A. Galeotti).
178.| ——zncrassata?| R. sulcata, var.
179.; —— mutabilis .| Cor.Cr.; Italy
(A. planata).
189.| d— obliquata .| A. Burtinii, var.
180.| td— Omalii ...| J A.undata, Gd.
182. sulcatanerelin |) beceseeest
173. triangula-| A. minuta ......
ris.
167.| Cardita chame-| C. scalarts, var.
formis.
168.)d-— corbis ...) «ss.
167 orbicularis|) __.........
166.) t—— scalaris ...| C. borealis, Con.
165.| +}d— senilis ...| C. suleata, Brug.
Cor. Cr.
157.| dCardium an- | C. edule,monstr.?|
gustatum.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK.
Class II. ConcuirErRA.
481
VOL, XXVII.—PART I.
veces
Vv. VI.
Localities.
Geographical 8p |
distribution. oO cE!
as} q
Oo °
Fa A
BSM j|SBW BtBr Ad C
godopodRb een WwW tapes
M iS) N E Th
SS VE Wile ere Ad
gaadonaeEens. ||) dadooc Ad
BSMWAt;} SBt | BrAd
BSMW |SBW Bt Br
sewnadeataae..”, Po batees Ad
BMWAt |SWBt| ......
BSMWAt| SBt | ......
BSMW |SWBt| ......
BSMW WwW N?
RR soos STEM IUAR © cocaine
Bt Wad
SPAT Whallte Miers PBrTAd
ceelete sect S Bt Br.?
BSAW |SABW|BrT Ad
BtFhWd| #
SA SW Stone
BMW |SWBt| ......
Bw SIAe IN Weve ste Br
Biabcbseb ott SBWd| TTh
dadoneooaaa6 S Wes
wddettaicens SAB wisidalas
Beers ak SWBWad\ ......
Am S Wd Br
BSAMWAt iS) Br T Ad
BMW At We vipers
Andaadooeshc SW sae000
M W At W Bt N
Pai aaseluewae S W ahs
Am SW NC
M W SBF Bt ......
SODACOBBURE SBRA Th
Bt
Monte Mario,
bf
bd
Italy.
et
974.| d—— striata
Page of Mo-
nograph
482
II.
Names of
Species.
.| Cardium decor-
ticatum.
echinatum
.| d-—— edule
.. —— greenland-
icum.
.| t—_ interrup-
tum.
..—— nodosum,
S. Wood.
—— nodosum,
Turton.
.| d-— nodosulum|
.| td— Parkinsoni|
strigillife-
rum.
.| ——— venustwm
2.| Chama grypho-
ides.
.| Circe minima...
.| tCochlodesma
complanatum.
.| Corbula com-
planata.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Concurrera (continued).
III.
Synonyms and
critical remarks.
C. norvegicum,
var., Spengler;
Cor. Cr.
C. norvegicum,
(C. oblongum).
C. fasciatum,
Montagu.
C0. Parkinsoni,
Jun.
C. Nuttalii,
Conrad.
eaceeeeee
C. norvegicum,
var. rotunda.
Corn@rweerecs
Cytherea trigona
Thracia prezete-
nuis, Pulteney,
var.
G. Corbulomya
...(|C. gibba, Oliv
(C. planulata)
958.) —— tenuis ...) — .........
134.| Cryptodon sin-j —.........
uosum.
Cultellus pellu-| Solen pelluci-
cidus. dus, Penn.
196.) Cyprina island-} _—_..........
ica.
197. TATSINGA), crcl (COR, Chee coodasnos
208.) Cytherea rudis | G. Venus (V. cy-
cladiformis).
146.) }Diplodonta ? | D. trigonula,
astartea. Bronn.
145 dilatata ...|D.rotundata,var.
Cor. Cr. (D.
Woodt).
144.) —— rotundata | Cor. Cr..........
J | Donax politus,) (D.vinacea)Cor.
220. Poli. y,
219. trunculus
Percssses
IV. Wo
Pome Geographical
of | distribution
depth. i
L-D | BSMW At
Lt-L; BSMW
C aw
L-D| BSMW At
L-D | BSMW At
L-C | BSMW
hues Am
C A
Lt-C MW
L-D | BSMWAt
It-D| BSMW
Lt-D| BSMW At
Lt-D BSAMWAt
L-C | BSMW
Lt-D BSW
ee ey
C-D M At
L-C | BM W At
It-C |. BM W
Lt-L| B
VI.
Localities.
=
3S |
5 Eo
BE aaa
Seiden bean Gne
Passim | Passim
SBBt | P BrC
Ad
SiBtaailwe eases
SAB Ad
ABA rie. «| Peueincss
S
SEW OP
Saat Ad?
SW T?
SOW? ol eae
Ss) aD)
W Ad
SW? Bt eee
SBW |BrN Ad
Wd Bt Th
Ween aeeeee
a sbaes Ad
ae Ad
SBA | Passim
F Bt
SB Widleelki see
SW Bt N
S Bt Br
S L
SHB ta Pees
SW oe ase
N) Th?
Vil.
| Coralline
So con
Vit.
Belgium.
se eeeele
seeeee
eeceer
eeeeee
eee eee
onte Mario,
Italy.
M
4
a
A
Page cf Ivio+
nograph
i
a
We}
—
a4
_
118.
92.
J
88.
90.
J 95
115.
116.
43.
45,
70.
J 71
137.
139.
148.
II.
Names of
Species.
.| Donax vittatus .
Erycinella ovya-
lis, Conrad ?
.| tdGastrana la-
minosa.
.| @Gastrocheena
dubia.
Glycimeris an-
gusta.
.| tdHinnitesCor-
tesyi, Defrance?|
disocardia cor
tdKellia ambi-)
gua, Wyst.
d— suborbicu-
laris.
Leda caudata...
hyperborea,
Lovén.
—— lanceolata
—— myalis
pygmea,
vy. Minster.
tLepton deltoi-
deum.
—— nitidum...
+Lima exilis ...
Loscombii
fLimopsisaurita
t-— pygmea,
Ph.
Loripes divari-
cata.
dlucina borealis
Lucinopsis La-
jonkairi.
. .| (i. depressa)...
PRESTWICH——CRAG-BEDS OF SUFFOLK AND NORFOLK.
ConcHIFERA (continued).
III.
Synonyms and
critical remarks.
A doubtful iden-
tification; Cor.
Cr.
G. guinaica,
Chemnitz (Fra-
gilialaminosa).
(Ofori (Ore; Ganandonc
G. siliqua, Ch...
H. giganteus, P.
Carpenter ;
Cor. Or. ?
Seintilla pari-
siensis, Conti,
non Desh.
Nucula arctica,
Broderip &
Sowerby, uot
Guid
(L. Phillipiana)
Erycina Geof-
froyi, Pay-
raudeau.
squamosum,
jun.
inflata, La-
marck.
L.
L.
(L. subleevigata)
Cor. Cr.
(L. anomala) ...
L. divaricatus ...
(L. flandrica)...
¢ Venerupis de-
cussata, Ph. ;
IV. V.
Zones G :
eographical
of distribution
depth. | ~~ P
lt-L | BSM W
Roses South Africa
L-D | BMW At
L-C A
Baan Am
L-D |BSM W At
C BM W
Lt-D | BSMW At
C-D BS AW
C SA
sees A
2 AA Am
C-D |BSAMW At
MW
BS W
M
BSMW
BAM W At
M W
BM W At
BS M W At
M
Cor. Cr.
VI.
Localities.
2 | a.
2 ER
3 bo
iat ZB
Ny Br P Bl
Ad
IVa Ma sce
SEARBAVVnesaeen
Wa
SiWidlua) wesc ae
S N
Trimley| TT?
SS) OTE ty pena
SWBt]| C Ad
WieWidisineensct
Si esltua eaues
Btadalim east
B Bt Br C
S Bt |PBrBlC
Ad
W Ad
NS)
Seaaito Ad
Waris Aller?
VV ivoks lat aera
Wilts 4h tiated
IV 2 cE VV(Cl eee
S Bt |BrT Ad
Passim | Passim
PS eeces
483
Coralline
Crag.
sn etee
wanes
eee aete ees eel eotene
seseee
sa eeee
Monte Mario,
Italy.
484
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Concuirera (continued).
me
Page of Mo-
nograph
II.
Names of
Species.
Lucinopsis un-
data.
.|Lutraria ellip-
tica,
3.| Mactra arcuata
constricta
deaurata
.| d-—— glauca ..
obtruncata
.| d— ovalas......
procrassa .
.| —— stultorum
subtrun-
cata.
.| d— truncata .
.| Modiola barbata
.| d—— costulata .
.| ——marmorata
.| —— modiolus..
dModiolaria Pe-
tagnee, Scacchi
.| dMontacuta_ bi-
dentata.
ferruginosa
.| —— substriata
.| Mya arenaria ...
.| d—— truncata...
.| dMytilus edulis
and var. hes-
periana.
| td@Nucula Cob-
boidize.
.| d— levigata...
5.| ——— nucleus ...
.| d~-— tenuis
.|dOstrea edulis
.|—— princeps...
.| Pandora pinna
.| dPanopzea Fau-
281.
jasil.
—-~ norvegica
Til.
Synonyms and
critical remarks.
M. glauca, var.
M.solida,monstr.
.\M.solida,monstr.
M. subtruncata,
var.
M. solida, var.
elliptica.
M. solidissima,
Ch. ; M. pon-
derosa, Ph.
eee eeseee
een essees
M. solida, var...
G. Mytilus......
G. Modiolaria...
G. Modiolaria...
G. Mytilus
sec e enone
ence eeeee
eeecescen
Gould.
oeeree eee
P. inzequivalvis,
L., var.
Cor: Crise.
G. Saxicava
IV. We
Zones fe :
eographical
of distribution
depth. :
L-C | BSMW
It-L| BS MW
tas) Bae secon ecae
Lt-L SA
Lt-L BSM
Lt-C | BSMW At
Lt-D|} BSM W
ttl | BMW
lt BM W At
L-D |BS M W At
Lt-D BS W
L-C M W
L-D|} BSM Ww
LD; BSMW
L-D BS M W
It-L | BSA W
Lt-D|; BS AW
Lt-L BS A MW
L-C | Japan.........
L-D | BSMW
C-D (BSAM W At
It-D| BSMW
LtD|BSA MW
At
C-D BSA
VI.
Localities.
ro)
3 a
Spiers
e 386
Fa aA
ed Ad
Sin ies.
SBW |PE Ad
SBE Rocke
SHEN
IND WG) sdcoce
Sirs ail Peace
BS Wd\ Br C Ad
| Btw N Th
FWd |...
Ss Br T Ad
S) Br P
S?Bt |Br Bl Ad
SUV wl “aresee
CVV fu alliiaseetee
W Wd Late
‘W C
Ss P Ad
Wd!) & ke
W Ad
sone Ad
aie Ad
S B F Bt} Passim
SB Wd |BrBICAd
Bt
SBWd | Passim
R Bt
SBT F| Passim
Wd Bt
WWdBt| ......
SBWd| ......-
Bt
B Wd W|BrC BAd
Passim N
S)INIB I sonccs
Wi tea
SiPAGIWicll| eee
S Bt Br C
Coralline
See) ees
Italy.
| Monte Mario, sl
II.
Names of
Species.
Panopiea plicata,
Mont.
.| Pecten dubius...
PRESTWICH——-CRAG-BEDS OF SUFFOLK AND NORFOLK.
ConcuiFERA (continued).
III.
Synonyms and
critical remarks.
q (Saxicava? fra-
gilis) Cor. Cr.
gracilis ...
d—— maximus
3.) d-— pusio
.| d-— tigrinus...
.|@ Pectunculus
.| d~— opercularis
.| —— princeps ..
—— septemra-
diatus, Mill.
glycymeris.
pilosus, Z.
FEholadidea pa-
pyracea, Tur-
ton.
.| @Pholas crispata
d—— cylindrica
— dactylus, L.
d— parva, Pen-
gant,
Pinna rudis, L.
.| Saxicava arctica
d-— rugosa ...
fScacchia ellip-
tica, Se.
dSolen ensis ...
d—— gladiolus..
d— siliqua ...
.| (Tapes pullastra
.| d-— texturata?
d-— virginea...
Tellina Bene-
deni.
balthica,Z.
.| d—— erassa......
.| d—— obliqua ...
(P. radians)Cor.
Cr.
P. oper cularis,
var.
(P. grandis) ...
Se i)
P. islandicus,
cece eeree
Cri)
eee eeetes
© sees ccves
ea ccceres
wee teerce
weceeceee
Oe irr
eer ecesee
eee eeeece
eae e wees
T. aureus, Gm.
T. virgineus ...
T. calcaria, var.
eect eenee
eee scesee
T. calearia, Ch.
EV.
Zones
Lt-L
L-D
T. calcaria, var.) ......
(I. ovata).
485
V.
Geographical
distribution.
BS MW At
BSMWAt
SA Am
BS MW At
BSMW
BS W
BS M W At
eee eet ecene
Vi. VIL.} VIII
Localities. f
sb #7 : Belgium.
s So jst jj.
o ss Zb = &p n nn
= | so |clesle:
= A Oo (hf m| as
ODDOOs, wal) aspoodde lalloesscdqel bdcodc *
SUN B Bt ecse.- * * x
[oie (7241) a eens eae a eb Lem ar | ea
W Bet
SPB avVidll ieee. x lox] x
Passim | Passim | x * *
Wd T Yarn | x * *
S BW N x [ox] x
Wd
1 oieekiell i. Meneses gel eee OEP lLooane
SBWBt) Br Ad | x fox] x
Passim | TBrTh} x }...... *
Wich reoiatyse Pe cil egal
Be aamilll tates ie * Qhiliveves
SWwWd!| PW tS REE AN e
Bt
EVA calibesecicss Fall | acssvel a eearae
War a ichaciea lee eee pee cee ee sos
AEN UR BBs a eee ett *
SWE SPF cases | eoeee a eG om [ecto
ISIE eis Gesoae x fox] *
SW Wd!Br T Ad} x» Jox|......
Bt
Bite Bierce) sl osacec[eesees | eames
SW Wd_|_....... x Jox| x
Bt
SOWVABE ee ae seule
SWd |BrTAdThi...... x | x
Wid lere ecard) ieee Mate er aT
W Wd a 63 ame ial eh tal ba Reee
S W Br came | (Sane *
Soha hi ald oveieoe sa | ee * | x
ae Ree) Walgse e ae
SW Bt; TPC] x * *%
Ss bRe BIB eA eee lies
Ss 183 (OTB eee | Scugallooonne
: Ad ae
SBET\BrPBi * * | *
Wd Bt | Ad Th |
IX.
| Monte Mario,
Italy.
486
PROCEEDINGS OF THE GEOLOGICAL SOCIETY,
ConcniFEra (continued).
|
I. II. Ii. IV. Wo VI. VIL VEEL. |) ix
; Localities. Beloi Si
e) - : eleium
=] Names of Synonyms and ei Geographical op s g 5 Ss ;
os Species. critical remarks. distribution. 5 ‘sap |S ap @ be
@, & cepa. s Pe les18 .|28las
Ie) i) ma\seslou
a Fe Pn Sie Se
230.| dTellina prete-| T. calcaria, var.) ...... | sscceseeeees SW ¢ 3 Bre BOC) time x | %
nuis. Wd B | Ad Th
300.|Teredo norve-| ......... Lt BSM W 2818 | cocoon radius ll 8
gica.
261.) Thracia inflata..| T, Conradi, C Am Bwae 9) istinese Pon). Beene %
Couth. ? (T. cor- :
buloides, Desh.).
260.) -—— phaseolina|'T. papyracea, | Lt-D |BS M W At| ...... Ad x f * | x
: Poli.
235. 'Trigonella plana Scrobicularia pi-| Lt-L | BS MW Ss? Br ‘€* | verccel vere saeco
_perata, Belon.
205.) Venerupis irus.. paeacue L-C | BMW At NSN caased Peers Bec assoc
210.|dVenus casina | (V. sulcata) .... L-D |BS M WAt|SB oa Jonnie * [-* | *
Wd Bt
J |d-—chione, Z| (Cytherea chio-| L-C | BMW At Well. ccades eae ox] * | x
207. noides).
211. TEISOIENEN sacl) anaononac Lt-D |BSMWJapan!S W Bt| Br |......)......).....- *
212.| d-— imbricata..|V. fasciata, var..| 0.0... | s.sececeneee SUG ON ta eee Je ikciewen eae +
213.) —— ovata ...... Cor, Ge cétvsscoe L-D |BSMWAt] S Bt Ad x fx | * | x
Class III. Sorenoconcuata.
188.) Dentalium cos-| D. dentalis, Z., | L-C MW SEB tre ei aoe SE POL seal Seneae +
tatum. yar. ; Cor. Cr.
J abyssorum, 200000 C-DIBS A MW Atl 20 cece. d! deemeeet aeeenl Beeteee
Sars.
Class IV. GAstropopa.
J |Acteeon exilis, J.) ......... D M At We een
169.) —— Noe ...... qA. pusillus, D M At Bw W B
Forbes.
170. —— subulatus..| A.tornatilés,var.| ...... | scecceerenes S Bt Br
170.| —— tornatilis.) —......... Lt-D| BSMW S Be |BrPBIE
Ad
139. Adeorbis _ sub-) (Trochus trigo-| Lt-C | BM W Sah Goll take ves
carinatus. nostomus).
Asmenuie, C298= |) coonecoce Cc A Am SE) POL iscncine
dida, Moller
25.) Aporrhais pes-| (Chenopus) I-D| BSMW |SNBw Th
pelecani. B Bt
34.) Buccinum Dalei| G. Buccinopsis | C—D BS SW Bt; ECP
J ORIEL oa3coaden. 2 | sococee A NM, dara tates
J |—— pren- | a... Lt-L A Bt NEC
landicum, Ch.
3D. undatum..|(B. tenerum) ....| Lt-D| BS W SBtNW(|N ECTh
175.| Bulla cylindra-|G. Cylichna ....| L-D | BS MW At] S Bt Br
cea.
173, lignaria...|G. Scaphander..| Lt-D|} BS MW | S Wd
PRESTWICH — CRAG-BEDS OF SUFFOLK AND NORFOLK.
GastTRoPODA (continued).
I II.
fe}
S| Names of
|S 2
[os Species.
a8
3 a
(AY
177.| Bulla regulbien-
sis.
176.) —— truncata ..
116.| }Czecum mam-
millatum.
159.) Calyptrza chi-
nensis.
64.| Cancellaria co-
ronata.
66.; ——costellifera
65.| t-— mitreefor-
mis (?)
156.| Capulus milita-
ris.
156.) —— obliquus ...
155.) —— ungaricus
97.| t? Cassidaria bi-
catenata.
J 71.| Cerithiopsis
Metaxa, Delle
Chiaje.
70.;—_—tubercularis
72.\ Cerithium ad-
versum.
73.|t-— granosum
reticulatum,
Da Costa.
69.| -—— tricinctum
70.) —— trilinea-
tum, Ph.
69. variculo-
sum.
80.) }Chemnitzia
costaria.
J 82.) —— densecos-
F tata.
81 elegantis-
sima.
J8l1 interno-
dula.
63.| Clavatula Boo-
thi.
61.| t—— _cancellata
61.| +—— concinnata
III.
Synonyms and
critical remarks.
Utriculus obtu-
sus, Mont.
eeereeree
C. yaricosa, Bre.
Admete viridu-
la, Fabricius.
(lore, (Or, Goosooses
C. ungaricus,
jun.
Y a7,
C. ungaricus,
var.
C. ungaricus....
C. tyrrhena, Ch.,
var. ?
G. Triforis; T.
perversa, L.
beet ences
(C.Woodwardi)
(var, inversum)
C. reticulatum,
var.
G.. Odostomia ;
Cor. Cr.
O. rufa, var. ...
O. lactea, Z. ...
qC. corbis, Conti
Defrancia Leu-
froyi, Michaud.
D. reticulata,
Renier, var.
Pleurotoma de-
Vy.
Geographical
distribution.
oo eseeeoeses
Bee eeseeeeae
BS MW At
M W
BS MW At
BSM WwW
M W At
cussata, Ph,
VI.
Localities.
Bente”
) iS +
Br P Ad
Beane Ad
Sian lites
Passim |Br P Ad
Th
VV VG eerie
S Bt Wd Br
Soot a AAS
ISNA eee
SWNB} Br Ad
Bt Wd
SBF 9
Wipe acon
NS) Br
Wits biioessace
NYG Gili gee
Bt W N
Passim | Br T Ad
Th
IVE beau ea
Wee tee ccce
Beeinsiway tse
W
W Bt N
S Bt Br Ad
SOW Glee:
gaan: || ene
Sieealiesenent
487
oralline
_Crag.
| C
SOOO odor
7 | Montini.
Ttaly
iS
a
nograph. =
Page of Mo-
58.
-| Erato levis
.| —— polita
Maugeriz
tEulimadistorta
intermedia,
Cantraine.
Fissurella costa-
ria, Basterot.
preeca
Fusus despec-
tus, Z.
t-— Sarsi, J....
Hy drobia ulve,
Penn.
Lacuna crassior
divaricata,
Fabr.
Lepeta czea,
Milt.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
488
II. Ii.
Names of Synonyms and
Species. critical remarks.
Clavatula cos-| G. Pleurotoma
tata (?)
levigata(?) » »
.| —— linearis ...| G. Defrancia ...
mitrula ...| P. costata, var.
nebula ...| G. Pleurotoma
plicifera...| P. elegans, Mol-
ler ?
Trevelliana|P.turricula,worn
.|—— turricula...| G. Pleurotoma
Coltmmibelllai|eeeeeeeee
scripta.
| == SURE, Go} aoc ogaoes
tConopleura |] Pleurotoma
Maravigne, incrassata,
Bivona. Dujardin ;
Cor. Cr.
.| Conovulus my-| G. Melampus...
osotis (?).
pyramidalis| ,, 5
.| Cyprea anglie,| C. retusa, var...
-|——ayellana...) .....-...
europaea |) | weescees:
o| == TREE) Goal) deaddooan
tDefrancia hys-| —.........
trix (Jan),
Bellardi.
.| Emarginula (E. fissura) ......
crassa.
SOU), “Goul| | osacnogod
G. Marginella
lor, Cle scoadso
eee ceenee
Perc eweee
Desh.
eae creeee
eesccccce
Gastropopa (continued).
eeeeee
@eeene
V. VI.
Localities.
Geographical ep a
distribution. o) =
; = 5
o fo)
fan A
BSMW |SWBt| .......
BMW At | W Bt | .......
BS MWAt|S W Bt} Br Ad
Aco notes S W Bt
BSMW Siac alleeacneeee
BS Siwy Galemecceae
Stata cen S Br
BSAW (|SWBtEh|Br Th Ad
M W SW Wd_ ......
Rea ecetistice W Br
M W Sia coe
BM W iS) Br P
Ae ee cae S Bt | BrETh
eG One S sities
He eM rs. S W Bl
BS MW | Passim “il
so hanaean eter: Ss) wasn
M At Wate Alanson
BS At SiN iieleeecsene
BS MW At| Passim | _......
BMW Ss N
West Indies See viiilleri scars
BS M W At Witrit eds tae
BSMW At VE cai Selecta
BS MW W Br
M Wd btenat
BMW At SHB at) nest
W Bt
ABS N) Br Th
BS At Bt Wd | ......
BSMWAm| W BrT Ad
IBUS GAN) uiltanseeeee Br
BISA Amy |) ieee Br
BSA Wi ecileee
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK.
GASTROPODA (continued).
489
ik II. TTI. IV. V.
lo) =
= =| Namesof | Synonyms and FERS Geographical
ws . 2: (0) : . .
os Species. critical remarks. Hecke distribution.
S eu ep °
aa
Ay
118.\laittorinalittorea) —......... Lt BSAW
p—eBUGIS, = |). cevcecee's Lt BS AW
Maton.
120.| -—(?)suboperta| L. littorea, var.) ...... | .csceseeeess
J | Mitra corni- | M.ebenus, Lam.| C M At
cula, LZ.
J |Menestho al- | _......... C A
bula, Fabr.
40.| {Murex tortuo-| M. erinaceus, | Lt-C |BS M W At
sus. L., var.
32.| Nassa conglo-| Desmoulea ab-| ...... Africa
bata. breviata, Ch.
31 CONSOGLOEG| NCIC ANST UAT ecw. ||P eeceaueeene:
J |—— Cuvieri, | —......008 C MW
Payr.
30.} t—-- elegans...) «........ C-D W At
29.| -—— granulata| .......... C WwW
28) HMCTASSAtAl | |. eeeeee ss Lt-D | BS M W At
28.| t—— labiosa ...| N. semistriata,| C—D MW
Bre. ; Cor. Cr.
aa —— monensis { a wee, GSsaut; Bab Win Mea SCNee
32. prismatica| Not N. prisma-| C-D MW
tica, Br., but
N. lima seu
limata, Ch.,=
N. scalarifor-
mis, Kiener ;
Cor. Cr.
30.) -—- propinqua| N. trivittata,Say, Lt—L Am
J |—— pygmea,| .......... C BS MW
315.| Lam.
33 reticosa ...|(B. elongatum)) ...... aioeenye
J | Natica Alderi,} — ..:...... CD} BSMW
Forb.
142. catena .../(N. Sowerbyi) | Lt-C| BS MW
141.) +-— catenoides| N. heros, Say? | L Am?
145.| +—— cirriformis| N. sordida, L-D| BM W At
Swainson.
147. clausa ...|N. affinis, Gm.| C-—D BSA At
146.) —— grenlan-| ......... C-D BSA
dica, Beck.
142. Gulle= WING ica teman jis | eeecee || teeters
145.} —— helicoides/N. islandica, Gm.| C—D BSA
144. lhemiclausall),: Wee San tel aeceeeaaen sa
148.) —— multipunc-| N. millepuncta-| C
tata. ta, Lam., var.
143 wartans ...| N. cirriformis, | ....02 | sccccevec ers
var. ; Cor. Cr.
VI.
’ Localities.
= a
Seep
SBBt | Passim
Bee BrT W
SAW EBa leases.
Wid eeekec
VV Fie eae
SW Bt Br
W
{San Mees
IBGAceliteieecn ss
WBE tll tek
Passim | ......
S Bt Wd) Br
SHB Gae| Gress:
ISBGE it Rees
Sion Tees ome
SW Bt! BrE
Bt Sasaee
Passim TH
S Bt Beats
S Bt |BrBlC
S W E Bl
SAVGL ih -seseee
S Bt |BrC Ad
S Bt | Br TW
S Yarn
S Bt |BrE Ad
S W N Bl
Wis Ghillie eee
SAGs all faneeeee
Monte Mario,
Italy.
*
2K
490 PROCEEDINGS OF THE GEOLUGICAL SOCIETY.
GASTROPODA (continued).
Ip Ii. ie IV. Ve NV VIL|P VEL axe |
s Localities. 0 ig :
= S| Names of Synonyms and none Geographical 2 = Ss ems Ss : |
Ss Species. _ critical remarks.) 5 O11, | distribution.| ‘So [2 etl ge
2, 5 oe 3 | 88 [Bolsa
ae @ (2 |S eer
J |Odostomia aci-| ......... O-D | BiSM IW At] W_- |), ...... dpe |
cula, Ph.
Tt — "acuta, Jes vectn dene L-C |B SM W At AVY coll ducers ee Bid] eee a a
J COnOIGeAay|||\ eee ee cee L-D |BS M W At WwW Br... capt eee eee
SLA Br
J |——interstinc-| —......... Lt-D| BS MW Wd | |. .ss.cc. Gee ees eee
ta, Mont.
J 85.) —— plicata, |(Tornatella co- L BS MW WW cll a ibe x fo} x |x
Mont. noidea)Cor.Cr.
A (ey CRIME eT anenddon D-D M W W Bo) 4 ete. (lace eee eee
Bre.
Bef | ——$—= ANCE! = so og0 ae C-D |BSM W At AWG a Wien eria vane * * *
14./ tOvulaLeathesii) Bulla spelta, L. C M W Bt Br? rane ee! * *
183. |Patella vulgata} ......... Lt-L|BSMW At} S Bt Assam Mees | Booaballssacrs:
J |Pleurotoma bi-| ......... C-D S At Am Bt | ovssost Uclb eee come eee
earinata, Couth. s
54.) t-— carinata...|Cor.Cr.(P. mo-| D-D | BS MW At} S| ...... 3s eat |e
diola
J harpula- ia ie C-D S At Am Bobi ty |gpasssose | Sse al ea
ria, Couth. J
53. TDOGRGTUETHIopelieu Ae anacile ee teu Neal ema ee NE once nach SB Ga Vidi aire ee aean eee Ox} x
J == fyaMIS NI Gdoecaeor — S Am Fh Ths a eee cee
dalis, Strén.
61. rufa, Mont. aiciedor as LtC} BSMW Bt i ae econ Pecceel haa.
54.|—— semico- | P. galerita,Ph.?| D? B At? SS) age iaeiieee am aceon Ie eeer *
lon.(?). Cor. Cr.
J |—— striolata, | ......... C BS M W Soe lege eee Be Pesgaraleess
Se.
53 TUErTe lay NOt Es turricullas ieee | aneeeeeeer iS) 18} 18}5 |) Jexe ox} x
Mont. (P.tur-
rifera).
J) =——" viaolacearl © tessceeeee Cc S A Am Bt Wd Pa: sl se ee eee
Mighels§ Adams.
36. Purpuralapillus| —......... Lt-L | BS AW At | Passim | Passim |...... x | o#
38.| ---— tetragona | P. lapillus, var.) ...... | .ceeeceee 0 SW Bt INOS Al sees x | x
J |tPyramidella | (P. plicosa) D-D MW Wie Pas dasa % cfu@hylaemeae *
uniplicata, Cor. Cr.
Duy.
P.subinterme-
42.&| | Pyrula accli-| } dia, Bronn ; e
aia | a Tee Cee oe WWdEt! ...... 2 tone are
reticulata).
22.) Ringicula bucci-) R. auriculata, | C—D M W At S Bt |YarnAd/ x Jox] * | x
nea. Menard.
22.) t-—— ventricosa} —_.......... D M At 8) Bt. | Br QD Ady seq iteces|eces: *
1O4:| Rissoa} (Con finis||) Yrs see eae eee meceesaenc eo coal neers Br Sa Pentel Aono
104.) ——pulchella(?)} Not Philippi’s] ...... | ........-- S BR Bb ies) lpseeee eerie
sp. ; R. curti-
costata, S. W.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK.
GASTROPODA (continued).
491
ili inl
}
a =| Names of
of Species.
1o x
Be
J |tRissoa Stefa-
nisi, J.
J striata,
100.| Adams.
J |——zetlandica,
101 Mont.
94.) tScalaria cla-
thratula, Ad.
J it communis,
Lam.
J 91.) t—— fimbriosa
93.| —— foliacea ...
90.) —— greenlan-
dica.
J pseudosca-
laris, Br.
94. Trevelyana
J |—— Turtone,
Turt.
J 90. yaricosa...
161.| Tectura virginea
26. Terebra canalis
26.) —— inversa ...
129.| Trochus Adan-
soni.
131. —— cinerarius
131.| —— cineroides
125, formosus
127 granulatus
Born.
J |—— grenlan-
dicus, Ch.
130) —— Kacksiz ...
J |—— millegra-
127.| nus, Ph.
129.} —— Montacuti
TINE
Synonyms and
critical remarks.
R. costulata,
S.W.notAlder;
Cor. Cr.
sect e wees
weet etsee
aescenees
eoereeres
Turbo lamello-
sus, Brocchi,
var. ; Cor. Cr.
Cori@rse ace.
sec eeeeee
eeeeeneoe
eee ceenes
Not Turbo yari-
cosus, Br.,nor
S. varicosa,
Lam.; Cor.Cr.
T. inversa, var. ;
Cor. Cr.
Columbella mi-
nor, Scacchi ?;
Cor. Cr.
A doubtful iden-
tification.
T.cinerarius,var.
(TL. solarium).
T. occidentalis,
Migh.
eee eeeres
T. Adansoni,
var. ; Cor. Cr.
weceesece
A doubtful iden-
tification.
eens
seseee
ee eeee
Vie
Geographical
distribution.
M
BSA W At
BSM W At
BSM W
BSMW
BS MW At
eee ect eteee
VI.
Localities.
Ep 2
SHY Cr 6
o =
NAVE 2 Fa Se
WW NAVE SS seco
Seite N?
AY TAG Loy dele
Wood- | ......
bridge
Wd
N) N?
N) Br E Bl
Ad Th
Sudbyaiiieeccs.
NS) N Br Bl
Ad
Sudb Th
Wa VWideSil) gages.
SBBw Bt Br
Wats feck
Sieh p time
Soe ligne ees
SEWeBiaipe oct:
SWB ees.
Sa aot rial Mamas
WwWdeBt BrT
eit N
ESR ONE| lies Bakes
Sioa Bab sacne
VIl.g VIII. IX.
Hey AS
Belgium. [5
3 =.
= aS
i & 8 aS
ASS al/ssion
SOls2 iss
(Ss) A ase
coe reer hae
She | pod 2s4loeages
Ce ener ce
geal cs x | x
* fo x?).....
ner acane a
BASS Sooo *
Sees Sr i i *
Se ERE as ies 3
ae * | #
be Ca Seeauluteiese
x fx | x
x Tx | *
shintee x | x
a) eee *
hte Sree Aaeaict *
Be inh, Gee teens
ean (arly accion
Bea Boonen banc: *
492
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
GastRopopA (continued).
III.
Synonyms and
critical remarks.
(T. Dekini)
Not T. papillo-
sus, Da Costa.
Var. of last spe-
cies.
wee cecece
I. II.
}
="s,| Names of
St} .
o8 Species.
& &
oo
AY
127.) Trochus multi-
granus.
126 papillo-
sus (?).
126.| —— subexcava-
tus.
130. tumidus...
128,] —— villicus (?)
124.! —— zizyphinus
47.| Trophon altum
44,| —— antiquum
49 alveolatum
J |—— barvicen-
sis, Johnston.
49 consociale
48.| —— costiferum
—— Gunneri
46 elegans ...
46,| —— gracile ...
50.) —— muricatum
312.]/—— norvegicum
48.|/——scalariforme
312. Turtoni...
74.| Turritella com-
munis.
75.) —— incrassata
J | t——subangula-
ta, Bre.
118.) Vermetus intor-
tus.
J glomera-
tus, Biv.
J |—— triqueter,
Biv.
20.) +? Voluta Lam-
berti.
var. ; Cor. Cr.
T. altus ...-e.-e:
G. Fusus.........
eoocee
Cor. Cr.
T. alveolatus,
var.; Cor. Cr.
T’. costifer
T.clathratus,L.,
var.
Ff, antiquus, var.
Fusus curtus, J/.;
not Buccinum
gracile, Da C.
T. muricatus ...
G. Fusus ......
T. clathratus, Z.
G. Fusus ......
T. terebra, Z....
T.triplicata, Bre.
V. subcancella-
tus, Bzv.Cor.Cr.
VY. Junonia, ...
iC
eeccee
V.
Geographical
distribution.
Cee eeecerooe
BSW
ee ccececscee
Coe eeceeccen
Gulf of
Mexico.
VI.
Localities.
ap
Borel leeaep
=e | &E
fam qa
Soe aeetice
SENBBVVillgeeenne
Bt
SIE socane
S Bt |BrTAd
IS TRE Scenes
S Br
Bt Wh) Geer
Passim | Br T C
Ad Th
S Bw Be
Wi Sialbeeeeeee
[Sfereraltte eae
SWAY TBE sussce
serene N
Tt BG sien
Passim N
We Bt) eek.
SE N
B Bt Br T
Ri hilt Sober
NS) BrCBlAd
Th
Passim | T Br Th
NViciies | 2a
S Broms-| ......
well Bw
Wiley) |ie es
Fh Wd | ......
Passim N
VIL} VIII
Belgium
i>)
Heh
ee
ae18.| 88
oD] <-2|2s5
OWA &| HS
steetoiets Teall tatters
adoond *
3 Ree:
* Aol nietetsrate
Bocund * *
* 31 || 9
PRE) (acre eee
SE NNR Seale as
seeeel *
* * | x¥
x | x *
Bees * *
x foP x x
Ere) (aroma nace e
x |x | x
Italy.
Monte Mario, 4
| y
Page of Mo-
nograph.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK.
LAND AND ERESHWATER SHELLS.
Names of Species.
—_—————S=S
Cyclas cornea ..........0.00.0
Cyrena consobrina
eee eeccee
Pisidium amnicum
ee eeeeeee
eeeeee
Carychium minimum
Helix arbustorum... .........
INSTOIGE coconcedesacodsa:
—— plebeium
—— pulchella
Cee eer rer eeeeee
eee roeeeeseeees
SO iy
pereg TA cocscccccreccecoes
Paludestrina (?) pendula
subumbilicata
(?) terebellata .........
Paludina lenta
Se iii
eeeeee
SJOUROA OVS) Gocinocoondoooe
Pupa marginata, Drapar-
naud.
Succinea oblonga
—— putris
Peete rene eoesesees
Valvata piscinalis
cristata
wa ee ee eesccsessoce
Synonyms and
critical remarks.
Spherium corneum
Corbicula fluminalis,
Mill.
sere ecene scores
see teseee C8eee
eases ceeeser see
Cee i i)
...| P. terebellata, var....
Hydrobia ventrosa,
Mont.
eect ees ereeceos
ihiaia oo, Bae
weet eee assenves
Paes eee eeeavces
eee eeeresonoree
eae Cee sovcescos
Seca eee e ene see
Cec ccereeccesee
| Localities
in
Red Crag.
Geographical
Distribution.
Europe, Asia ...
Asia
Europe, Asia,
N. Africa, N.
America.
Europe, Asia,
N. Africa.
Europe, Madeira
Europe, Asia...
N. America......
Europe, Asia,
N. Africa.
Europe, Asia, N.
Africa, Madeira
Europe, Asia,
N. America.
Europe, Asia...
eeecceses
eeceeerre
aeeceseee
eee eeeees
eer eases cene
IDIDIRO}VNE) Gooonsace
Europe, Asia...
Europe, Asia,
N. Africa.
Europe, Asia,
Iceland.
Europe, Asia,
N. America.
Europe, Asia,
N. America.
Europe, Asia, N.
' &S. America.
Europe, Asia ...
Hurope, Asia ...
493
Localities
in Norwich
Crag.
Br
eee cceree
Since the preparation of the Lists of Mollusca appended to my
papers on the Coralline and Red Crags, Mr. Alfred Bell has published,
in the ‘Annals and Magazine of Natural History’ for September
1870 and May 1871, considerable additions to the Crag-fauna.
AS
regards the Mollusca, several had been previously communicated by
him to Mr. Jeffreys, who examined the specimens; these are incor-
porated in the above lists.
revision.
Others have not undergone the same
The names of all the species described by Mr. Bell as new
are here subjoined, with the critical remarks of Mr. Jeffreys as to
those of which he has examined specimens.
494 PROCEEDINGS OF THE GEOLOGICAL SOCIETY;
Coralline Crag.
GASTROPODA.
Admete Reedii.
Buccinopsis pseudo-Dalei (8. Wood). ,
Conopleura crassa. C. Maravigne, Bivona, =Pleurotoma incrassata, Dujardin.
Menestho britannica. Not known to me as recent; but query as to the genus.
Nassa pulchella.
Pleurotoma curtistoma.
Soe : All these are P. attenuata, var. tenuicosta, Brugnone ;
oe _{ and they are one and the same species.
notata. |
—— volvula. )
Red and Norwich Crag.
GASTROPODA.
Actzon? Etheridgii. A. exilis, /.
Capulus incertus.
Melampus fusiformis (S. Wood).
Menestho Jefireysi. Previously known to me as an undescribed Greenlandic
species. :
N aaa ypalevells (also Cor. Cr.).
Ranella anglica. Young; perhaps R. gigantea, Lamarck.
Crag not mentioned.
GASTROPODA.
Fusus cordatus. Terebra exilis. T, canalis, S. Wood,
Nassa densicostata. var.
Besides the above, Mr. Bell has given the names of other species
as found by him and his brother in the Crag; but Mr. Jeffreys
has not had an opportunity of examining the specimens. These
species are as follows :—
Coralline Crag.
CoNCHIFERA,
Pectunculus insubricus, Brocchi.
GASTROPODA.
Cancellaria Bonellii, var. dertonensis, Cancellaria contorta, Pasferot.
Bellardi. Nassa granifera, Du7.
Red and Norwich Crag.
CoNCHIFERA.
Nucula nucleus, var. radiata, Hanley. Pecten Westendorpianus, Nyst.
SOLENOCONCHIA.
Dentalium incertum, Gmelin.
GASTROPODA.
Buccinum ciliatum, Mabricius. Nassa variabilis, Philippi.
Columbella avara, Say. Pleurotoma Bertrandi, Payraudeau.
Cyprea dertonensis, Michelottz. gracilis, Ph.
Defrancia Philberti, Michaud. pygma, Ph.
Fusus Jeffreysianus, Mischer. Scalaria communis ?, Lam.
Largilherti, Pet¢¢.
PRESTWICH—CRAG-BEDS OF SUFFOLK AND NORFOLK. 495
In consequence also of Mr. Bell’s papers in the ‘ Annals,’ and of Mr.
Jeffreys having lately had an opportunity of examining the Mollusca
procured by deep-sea dredging in the Swedish expedition of 1869
on the Josephine Bank and off the Azores, I am‘enabled to add a few
more species and localities to the list of the Coralline-Crag Mollusca,
as well as the zones of depth and geographical distribution for some
species hitherto considered extinct. wo or three errata in that list
will also be noticed.
CoNCHIFERA.
Cardita scalaris ; C. borealis, Conrad: C; Am.
Kellia ambiqgua is not Erycina pusilla of Philippi, but Serntilla pari-
siensis of Conti (not Deshayes); the first of these names must
therefore stand. In the column of “ Geographical distribution”
add “At.”
Lima ovata (L. nivea, Brocchi) occurred in the Swedish expedition
at a depth of 790 fathoms.
L. plicatula (L. squamosa, Lamarck), add Gedgrave.
Montacuta truncata is a variety of MZ. bidentata ; but the shell figured
by Mr. 8. Wood as MW. bedentata is a distinct species, which Mr.
Jeffreys dredged in the last ‘ Porcupine’ expedition, and proposes
to name MV. ovata.
Pandora inequivalvis, var. pinna, add Gedgrave.
Thracia inflata is probably 7. Conradi of Couthouy (a North-
American species), and not 7’. corbuloides.
GASTROPODA.
Adeorbis pulchralis: Swedish expedition, 320-600 fathoms. Mar-
garita trochoidea of 8. Wood is the same species.
Cancellaria scalaroides (C. varicosa, Bre.), add Gedgrave.
Cassidaria bicatenata (C. tyrrhena, Ch., var.?), add Sutton.
Cerithium adversum (Triforis perversa, L.): ‘ Porcupine’ expedition,
364 fathoms.
64. Clavatula plicifera ; J Pleurotoma elegans, Moller: C-D; BSA;
S. Also Red Crag.
J. tConopleura Maraviqne, Bivona; {| Plewrotoma incrassata, Du-
jardin: C-D; MW; G.
Emarginula elongata, add Gedgrave.
Fossarus sulcatus =F’. costatus, Bre. §S. Wood figured two different
forms as /. sulcatus and var. lineolatus; the latter appears to be
F, japonicus of A. Adams.
Odostomia plicata, Montagu. This species must also be added from
Gedgrave and Sutton. It inhabits the laminarian zone on the
coasts of Great Britain, Denmark, France, Italy, and Algeria;
and it occurs in a fossil state at Monte Mario and in the Red
Crag. ;
Pleurotoma gracilior, A. Bell: Sicilian Pliocene; Gedgrave. See list
of Mr. Bell’s new species.
496 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Pleurotoma Reniert, Ph., add **D” and “At.”
P. striolata, Sc., is from the Red Crag, and not the Coralline Crag, at
Sutton.
Scalaria subulata is not a variety of S. foliacea, but is a distinct
species. Mr. M¢Andrew dredged it off Teneriffe, in from 40 to
60 fathoms.
S. varicosa is not a variety of S. fimbriosa, but is a distinct species. -
It is not the Zurbo varicosus of Brocchi, nor S. varicosa of
Lamarck.
Trochus millegranus, add “D.”
127. tT. multigranus: D-D; At; 8. Also Red Crag.
T. tricariniferus (recte tricarinifer): Swedish expedition, 340-430
fathoms.
Trophon costiferum (recte costifer): Swedish expedition, 110-3800
fathoms.
Add Vermetus arenarius, L.: C; M; Orford.
The above will somewhat increase the percentage of recent species,
but will not, in other respects, materially alter the tabulated results
given in my paper on the “ Coralline Crag.”
EXPLANATION OF PLATE XX.
This gives a diagram-section passing through the centre of the Crag district
from near Manningtree, by Ipswich, across the hills near Buckenham and New-
bourne, passing through Sutton, Butley, Chillesford, Aldborough, Sizewell, to
the coast at Dunwich, thence along the coast by Southwold, Lowestoft and Yar-
mouth to Hasborough and Bacton. A branch from the section is prolonged
inland from Easton Bavent across the hills near Beccles to Thorpe, near
Norwich. ‘The names of the towns and villages are given approximately.
The relation of the Coralline, Red, and Norwich Crags, of the Westleton series,
and of the Boulder-clay series is given generally, and in accordance with ob-
served sections referred to in the text and given in detail in the woodcuts.
CORRECTIONS TO PARTS I. anp II.
Page 121. It is possible that the estimate for bed “e,” may be 2 feet, and for
bed “d” 5 feet, too thick, which would make the thickness of
the lower division of the Coralline Crag about 40 instead of
47 feet.
», 9330, Add Pectunculus glycymeris to the list of Butley shells.
» 343. Add Mastodon (tooth) to list of fossils found at Sizewell.
» 044. For the freshwater shells found at Bulechamp and Easton Bavent,
see General List at the end of the third paper.
», 346. From some memoranda left by Capt, Alexander, it seems that a
portion of the jaw was attached to the Mastodon tooth found
at Easton Bavent, and that it was taken out of a spot 5 feet
above the base of cliff, and apparently in the clay and not in
the sands,
OF IPS Quart. Journ. Geol. Soc. Vol. XXVIJ P1.XX.
RRR —
e333]3S5SS5WWW EEE SS
Coveluthe iff
N BAVEN™
NW.
oy
t
wl Sees ~o432 ay 7 > Pus. 5 5
Scale. F Dangerfiele hth-Bedford S$’ Covent Carden
che ~ ST mile:
Fat
GENERAL SECTION FROM THE NEIGHBOURNOOD OF IPSWICH FO NEAR MUNDESLEY ON THE NORFOLK GOAST. Quart. Journ. Geol, Soc. Val
Ss
Bentley Tidliingstone eee ua the Bucdeshion Davies Valley, ot the Sit Sholishen, Bulley Chillesford- Then N
Deben
Diowavich, AutP Soutiuvold Cir Easton Bevant Cll Oveluihe Chir
Pahetield, Clr Lowestott Gorton Cliff Gorlestore ClfP Yarmouth Scralby Cli?
S eee ;
Winterton. (ltt Pauling Hasborough Cut? Bacto ClitP Pastow ChitP a
awe 6
BRANCH SECTION FROM EASTON BAVENT CLIFF TO THE NEIGHBOURHOOD OF NORWICH.
NW.
Valley of
the Yare
Eastin Bavent Clir love Hills near Beccles Aldety Thorpe near Norwich
6 6
J RTE borders Oey, WEEE Red Gag *
CE halk 13 Gulline Gag e
Westleton Sands & Shingle Gite
‘ Glacial series. 7
Upper Boulder Cay.
Boulder Sands & Grawels Scale. F Dergerfislé inh Redford $* Cornet Garden
Lower Boulder (ay. Vinch -/ mile.
A (hillestird. Cley-
SS hillested Sand
Forest Bed
oy
ne
=e
t
STOW—SOUTH-AFRICAN GEOLOGY. 497
2. On some Pornts in Sourn-Arrican Grotocy. By Grorer
Witttam Stow, Esq., of Queenstown, South Africa. ee Its
(Communicated, with Notes, by Professor T. Rupert Jones, F.G.S.)
[Read Nov. 28, 1870*.]
I. On some of the Formations of Port Elizabeth and its neighbourhood.
§ 1. The Jurassic Formations (pp. 497-514).
§ 2. The Posttertiary Formations (pp. 515-522).
II. On the Dicynodon-Formation ; its Forest-zones and other strata (pp.
523-534).
III. The Climatal Changes of South Africa, as indicated by its Geology and
Fossils ; and especially the Glacial Denudation of the Karoo Strata
(pp. 584-546).
Appendix.
Part I.—§ 1. Tue Jurassic Formations.
Introduction.—Whatever advances geology has made diene: the
last twenty-five years in South Africa (with which the names of
Bain, Atherstone, and Rubidge will be ever connected), it must be
confessed that we are but mere students in the elementary portion
of this part of the great “ stone book of nature;” and it may be
expected that every new investigation will bring to light facts, and
lead to conclusions, of which at present we have but a feeble and
imperfect notion.
To the present time geological knowledge in South Africa has
progressed but slowly. The great broad outlines of the geology of
the country have been traced by those whose names have been men-
tioned; but the minutiz have yet to be filled up. The South-
African explorer labours under many serious disadvantages, not only
from the horizontal position of many of the strata, but from the
want (with the exception of a few mountain-passes) of great road-
cuttings, and from the absence of mining operations, so that he has
to depend upon the escarpments found along the river-valleys and
mountain-sides, leaving large intervening tracts that must still re-
main in some degree of uncertainty until opportunities shall arise
for their more definite examination.
With regard to the fossiliferous strata in the neighbourhood of
Port Elizabeth, and of the Zwartkops and Sundays Rivers, for a long
time I had felt that too much had been done in the way of curi-
osity-hunting, by miaing and generalizing all the fossils of what
has been termed the “ Uitenhage Formation,” from whatever part
of it they may have come; thus shells from the upper and lower
parts of the Zwartkops River have been massed together, as well
as those from the Upper and Lower Sundays River, although many
miles intervene between the different localities—a plan that can only
lead to a confused idea of the different strata; and I felt certain that
this was one of the causes that prevented just conclusions being
arrived at with regard to the formation in question.
As a commencement towards getting more perfect results, I sepa-
* For the other papers read at this meeting see pp. 29-33.
VOL, XXVII.—PART I, 2M
498
(Section D of the Author.)
Fig. 1.—Collated Sections on the Zwartkops River.
W.
Cuyler Manor.
Rocke s Bluff.
Old Grahamstown Road.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Fn SI nn nn
~—=-—-—- Course of River.
No. 11. Cucullea-Kraussii-bed.
No. 18. Astarte-Bronnii-bed.
and Trigonia-Herzogit-bed.
No. 10. Ammonite-
No. 12. Hxogyra-imbricata-bed.
No. 9. Trigonia-bed.
rated the various fossils I obtained ;
and the longer I continued the ex-
amination the more I was con-
vineed that not much practical good
would be effected until not only
the fossils from each locality, but
also from each particular stratum,
had been separately arranged. In
this paper I record the results of
these observations, imperfect as of
necessity they are, doubting not
that future investigators, with
more lengthened opportunities
than I have had myself, will most
probably modify some of my con-
clusions.
A. Trigonia-beds of the Uiten-
hage Formation.—In following up
this subject I shall first treat of
the fossiliferous strata of the
Zwartkops River, and then of those
of the Sundays River. After that
I shall proceed to describe the
more recent deposits in the neigh-
bourhood of the former river and
Port Elizabeth.
Lower Zwartkops River. Section
at Rocke’s Bluff—trThe portion of
the Lower Zwartkops River that
has been most frequently exa-
mined is a part of the heights not
far from the mouth of the river,
named by the geologists visiting it
“ Rocke’s Bluff,” after our friend
and fellow-labourer Colonel R. H.
Rocke. It is situated about a
mile above Rawson’s Bridge, on
the east bank of the river. Here
the lowest fossiliferous band is
found in an old road, and is
marked No. 13 in Section A* and
fig. 1 (see also fig. 3). From it Isas-
trea Richardsoni + was obtained.
The most characteristic fossil of
this stratum is Astarte Bronnic.
Pleuromya lutraria and Astarte
* The sections mentioned but not
figured in this memoir are preserved in
MS. in the Society’s archives,
t Quart. Journ. Geol. Soc. xxiii. p. 162,
STOW——SOUTH-AFRICAN GEOLOGY. 499
Herzogu are rather frequent. The other shells are Gervillia dentata,
Pholadomya dominicalis, Hxogyra imbricata, Arca Jonesti, and an
Ostrea. In the bed, marked No. 12, near the upper part of the bluff
(figs. 1 & 3) we find Ewogyra wmbricata very abundant; Astarte Her-
zogtti and Pleuromya lutraria are numerous ; but of Astarte Longland-
stana only one specimen has been found, and one of T’rzgonia Cassiope.
The other fossils known to occur, in bed No. 13, are :—Arca Jonesii,
Cucullea Kraussii, Pinna Atherstone, Placunopsis subjurensis, Tri-
gonia ventricosa, T. conocardiformis, Ostrea, Pecten?, Ammonites.
No. 13 is about 50 feet above the level of the river, and No. 12 about
200 feet. The rocks in this section dip 2°-4° from the river in-
wards, and are surmounted by Pliocene (?) limestone.
Upper* Zwartkops River. Section on the Old Road.—Some miles
further up the river, on the old Grahamstown Road (fig. 1), above the
drift (ford), another fossiliferous bed (No. 11) is exposed along the hill-
side and across the road, as shown in Section B (fig. 3), some hundred
feet above the river. The dip of the strata here, said by Dr. Ather-
stone to be about 8°, isinwards from the banks of the river. Itis here
that Cucullea Kraussii is found more frequently than in any other of
the fossiliferous bands, together with Yrigonia Herzogii, Astarte
Herzogu, and Pleuromya lutraria, all of which are very numerous,
and may be looked upon as the characteristic shells of this stratum.
The Cucullea, especially, seems to have flourished at the time of the
formation of this bed, and must have grown to a large size, as its
fragments show. The other fossils are :—Pleuromya lutraria, Cero-
mya papyracea, Trigoma Herzogit, var., 7. conocardiformis, T. vau,
Exogyra imbricata, Pecten, Pinna, Patella.
Section at Cuyler Manor.—Still further up the stream, near Cuyler
Manor (fig. 1), is another exposed portion of this formation. I have
not visited this locality myself; but Mr. Longlands, who examined
it in 1867, very kindly furnished me with the section shown in
Section C (fig. 3).
In the stratum of friable sandstone, marked 10, he found Ammo-
nites, and very numerous specimens of Trigonia Herzogi; in fact
the latter abounds so much that it may be looked upon as the most
characteristic fossil of this section. He also found a few specimens
of Exogyra imbricata, and a few fragments of Trigonia conocardi-
formis and Pleuromya lutraria. ey
Remarks.—As the whole of the Zwartkops strata dip inland, and
along the course of the river, which has a somewhat rapid fall to-
wards the sea, I think these circumstances tend to prove that
these fossiliferous bands, as shown in Sections A, B, & C (fig. 3), are
not one and the same stratum, but form a parallel serves, asis shown
(in an exaggerated form) in fig. 1. Thus the stratum No. 13, in
which Astarte Bronnii abounds, must be the lowest; the bed, No. 12
at Rocke’s Bluff follows, with its multitudes of Exogyra; the Cucullea-
bed on the old Grahamstown road is the next in succession ; and,
* The word “upper” here used in reference to the Zwartkops and Sundays
Rivers does not indicate the highest parts of those rivers, but some portions to-
wards the furthermost range of the Trigonia-beds traversed by them.—T. R, J. -
2m 2
500 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
finally, the Ammonites- and Trigonia-zones of Cuyler Manor suc-
ceed ; and these positions, I believe, will be fully proved upon more
mature investigation.
Lower Sundays River. MeLoughlin’s Bluff, or Prince Alfred’s Rest.
—TI will now describe the Sundays-River strata, commencing with
those nearest the mouth of the river, and following up our exa-
mination along the course of the stream. The first section is that
of a bluff, about a couple of miles from the mouth, which has_ been
named by some of my geological friends “‘ McLoughlin’s Bluff,”
after ‘mine host” of a small inn*, now called “ Prince Alfred’s Rest,”
in the plain below. This Section, E (see fig. 3 and Sketch, fig. 2), is
the most marked of anyI have seen of the upper portion of the ** Ui-
tenhage Formation.” The rocks of this series appear to be superior
to those exposed along the lower banks of the Zwartkops, shown
in Sections A&B. Unfortunately, the lower part of the bluff is so
thickly covered with brushwood that no definite conclusion could be
arrived at with regard to the underlying strata; but in the water-
course of a somewhat precipitous kloof, at a little distance from the
bluff (see Section F) was found a lower fossiliferous stratum contain-
ing Astarte Herzogii, Trigonia Herzogu, and Pleuwromya lutraria.
This bed seems to be nearly similar to the stratum No. 11 (fig. 1) on
the lower part of the Zwartkops River. Intervening between this
and the fossiliferous band marked 5 in this-section (F), which bed is
evidently the same as that indicated by a similar number in Section E
(fig. 3), were sandstones some 250 feet in thickness; but here, as at
the bluff, the brushwood and débris prevented an accurate examination
* Formerly referred to as “McLoughlin’s Inn” in the papers by Atherstone
and Rubidge. The fossils from Sundays-River mouth and those from ‘“ Prince
Alfred’s Rest” (or McLoughlin’s Bluff) were unnecessarily separated in the
paper in Quart. Journ. Geol. Soc. vol. xxiii. p. 170.—T. R. J.
Fl [To face p. 500.
Fions A, B, C, E & F, and G.)
Upper SundaRiver.
Modder Id road
A).
|
Posttertiary ...........
Pinna Atherstonei,
Trigonia Herzo-
gu, and Astarte
Longlandsiana.
Ammonites suban-
ceps, Modiola Bai-
nit, and Gastro-
chena in wood.
Trigonia creo)
T. conocardifor-
mis, T. vau, As-
tarte Herzogit,and.
Cyprinarugulosa.
‘Aonites and Trigonia Herzogii, with, rarely, Exogyra wm-
icata, Trigonia conocardiformis, and Plewromya lutraria.
\llga-zone, with Cucullea Kraussit, Trigonia Herzogii, As-
rte Herzogti, Plewromya lutraria, Exogyra imbricata (all
mmon), Trigonia vau, T. conocardiformis, &e. (rare).
Zone of Exogyra imbricata, with
Ammonites, Astarte Longland-
siana, Trigonia Cassiope, and
Cucullea Kraussié (all rare),
and Astarte Herzogii and Pleu-
romya lutraria (common).
Zone of Astarte Bronnw, with
Tsastrea Richardson, Pleuro-
mya lutraria, Astarte Herzogi,
Pholadomya dominicalis, &e.
Fig. 3.—Obllated Sections of the “ Uitenhage formation” (Jurassic).
Upper Sundays River (Addo and
Lower Sundays River (ML -
odder Drifts) (Sect. G). eee onan
lin’s Bluff, near Prince Al
Rest) (Sects. # & F combined),
Red Marly Clay.
Posttertiary 4 Tufaceous Limestone.
ane~---—~------- Conglomerate.
Sa eea es Oyster-bed.
Posttertiary ...........
Few and small Tr7-
Fea eee gonia.
[me of Trigonia ven-
Pinna Atherstonei, tricosa and T. vau,
Trigonia Herzo-
gu, and Astarte
with Gervillia den-
3)
: 3 tata, Exogyra im-
Longlandsiana. g | bricata, &e,
8 F
2 | S=SSeeeeey G--------- Few Hamites and
Ammonites suban- g wood.
ceps, Modiola Bai- 5 m2 } =
Se eae i 2 : Co Ge
3 lemnites, Ancylo-
Trigonia Horaogii, \ 5 ceras(?), Drigonia
LT. conocardifor- 2 Goldfusst, Crassa-
mis, T. vau, As- oy tella complicata, &e.
tarte Herzogii,and 5
Cyprinarugulosa.
[Strata
hidden. ]
--— Astarte Herzogii, Tri-
gonia Herzogii, Pleu-
romya lutrari,
Lower Jurassic.
Se
eel ee ee
(Section H of Author, including his Sections A, B, 0, E& F, and G.)
[To face p. 500.
(Sect. C).
Upper Zwartkops River. ges ene River.
; ~ ke’s Bluff and old road
Cuyler’s Old Grahamstown es i
Monor Road ( Sect, B), below it ‘ Sect. A).
—— wenn nn nanan nen ‘Trigonic.
—' Ammonites and Trigonia Herzogii, with, rarely, Exogyra im-
bricata, Trigonia conocardiformis, and Pleuromya lutraria,
‘Cucullea-zone, with Cucullea Kraussit, Trigonia Herzogii, As-
tarte Herzogti, Pleuromya lutraria, Exogyra imbricata (all
common), Lrigonia vau, T. conocardiformis, &c. (rare).
Cee me meee Zone of Hxogyra imbricata, with
Ammonites, Astarte Longland-
siana, Trigonia Cassiope, and
Cucullea Kraussii (all rare),
and Astarte Herzogit and Pleu-
romya lutraria (common).
_Zone of Astarte Bronnii, with
Isastrea Richardsoni, Pleuro-
mya lutraria, Astarte Herzagii,
Pholadomya dominicalis, &e.
STOW—SOUTH-AFRICAN GEOLOGY. 501
being made. The existence of this Astarte- and Trigonia-band seems
to point out that the position I have given to the sections (on the
Zwartkops) is the most probable one.
The fossiliferous strata Nos. 6 & 7, in Section E (fig. 3), were evi-
dently deposited under very different circumstances from any of
the others ; and wherever the one I have styled the Modiola- and
Hamites-zone (No. 7) makes its appearance, it possesses the same
lithological character. I have given this name to it on account of
the numerous specimens of Modiola Bainw and fragments of the
Hamutes africanus found init. In this locality (McLoughlin’s Bluff)
this stratum is full of small fragments of carbonized wood, which
rub down to black powder under the finger. These minute frag-
ments seem to indicate that the sedimentary matter of which this
‘particular portion of the bed is composed, must have been the
deposit of some current of water laden with innumerable small
pieces of vegetable drift, such as we see washed up in the present
day on the seashore, after rains, near the mouths of small rivers.
Some miles further up Sundays River, where this bed is again
exposed, and where its thickness is much greater, these specks of
carbonized matter are wanting—an indication that this latter por-
tion was most probably deposited further off shore, or from a dif-
ferent direction; but I shall have again to allude to this in my
observations on the Upper Sundays River. The shells also of this
stratum are, with few exceptions, of a very different character from
those of the Astarte- and Trigonia-beds, the shells of the latter
being, for the most part, strong massive shells, fit to live along the
coasts of an open sea, whilst those found in the zones of which I
am now speaking are, most of them, thin and fragile. The rock
itself is of a much looser texture than the associated non-fossili-
ferous sandstones—while these latter, which intervene between this
bed and the uppermost layer, increase in friability as they ascend,
and show a considerable difference from the compact sandstones of the
Lower Zwartkops. The rock composing the Hamutes-zone is patchy
in colour, appearing in some places of a reddish sandy tint, but
more frequently grey. This was the bed (No. 7) in which the large,
coiled, broken fossil, thought to have been an Ancyloceras (?), was
discovered by Major (now Lieut.-Col.) Rocke. In no other, that
IT am aware of, haye Hamites africanus and Belemnites africanus
been found: fragments of the former are here exceedingly abun-
dant; but the latter is rare. Modiola Bainii seems almost ex-
clusively confined to this stratum. Fragments of either Hamites
or Modiola, found in the débris of the neighbouring cliffs, are
always a sure indication of the close proximity of this band. The
principal shells characteristic of this zone, are:—Hamites africanus
(very numerous), Ancyloceras (?) (two specimens), Trigonia Gold-
fussi, Tr. conocardiformis (young), Crassatella complicata, Modiola
Bainit (numerous), Mytilus Stowianus, Mytilus Rubidger, Belemmtes
africanus (rather scarce); also, I believe, Alaria coronata, and small
specimens of Astarte, Ciprins (?), Psammobia (?), and Ostrea (nar-
row, curved).
502 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
There cannot be the slightest doubt that, if future explorers will
-arrange the fossils they obtain from these different strata according
to the particular band from which they are derived, the scanty
lists here given will be greatly enlarged.
There is another somewhat remarkable feature in the shells of
this (No. 7) and the stratum (No. 6) immediately above it—namely,
that the large Trigonie are wanting, although there are numbers
of the smaller kind, and young individuals. Future investigations
will perhaps modify these conclusions. The Hamites and Modiola,
from which I have named the zone, may be found to extend into
others in reduced numbers ; but in this particular zone they have a
great numerical superiority.
In the bed marked 6, the same type of shells appears as in No. 7.
The rock is also apparently of the same kind. But only a few
small fragments of Hamites are found; and in the bed above,
marked 5, the Hamites seems to have disappeared entirely, and
apparently all the peculiar shells that accompanied it—their places
being supplied by others of a different character. Amongst these the
principal is the beautiful Trigomia ventricosa. It abounds here, and
is, In fact, the characteristic fossil of the bed in this particular
locality. A few isolated specimens have been found in the Zwart-
kops strata; but here they are, in some places, massed together in
thousands, outnumbering every other shell. Zrigonza vaw is also
very abundant; and hence, in the general Section (fig. 3), I have
ealled this (No. 5) the Trigonia-ventricosa- and T.-vau-zone. Fine
specimens of Gervillia dentata also have been obtained from it, toge-
ther with Hwogyra imbricata, Pecten Rubidgeanus, and Turbo
Stowianus.
In bed No. 4 the Trigonie, compared with those in No. 5, are
not only very much fewer and smaller, but, from some alteration
of circumstances, apparently were disappearing from this part of
the ancient ocean. The remains of other shells are also far less
abundant than in the lower zones. The sandstone above No. 4 is
much altered in character compared with those underlying it, being,
as I have before remarked, less compact, and far more coarse and
friable than those below. This difference of texture increases the
nearer we approach the upper portion of the section, where the
sandstone seems to assimilate in lithological character more to the
upper sandstones of the Koega, and to those interlaminated with the
clays at the Bethelsdorp Saltpan (see further on), than to any others.
Immediately above these, as shown in Section E (fig. 3), is a shell-
bed, from 3 to 5 feet thick, composed of small fragments of shells,
thickly interspersed with a species of Ostrea. This stratum seems to
be of Pliocene or Postpliocene age, and to be the equivalent of the
upper shell-limestone on the Zwartkops and the Koega. Above
this, again, is a conglomerate, varying from 8 to 6 feet in thickness.
This is capped with tufaceous limestone, from 2 to 3 feet thick ; and
above the limestone is a red, sandy, marly clay, varying, according
to the inequalities of the surface, from 4 to 6 feet. I send a sketch
of the bluff (fig. 2), the better to show the formation.
STOW—SOUTH-AFRICAN GEOLOGY, 503
Above the Modder Drift (Ford).—The country for a distance of
some 10 miles in a straight line between McLoughlin’s and Modder
Drift, on the Sundays River, I have not been able to examine; but
from the Modder Drift, for several miles, to the krantzes (precipices)
below the Addo Drift, at Tunbridge’s, three distinct fossiliferous
bands make their appearance at intervals—that is to say, wherever
the rocks are sufficiently exposed on the slopes of the hills that bound
the 8.W. side of the river.
Unfortunately, it is here the same as lower down the river, and
the hill-sides are too much covered with débris and brushwood to
enable any one to make a very accurate survey of the intervening
strata. The belts vary from 2 to upwards of 3 feet in thickness.
The lowermost, No 3 (see Section G, fig. 3), contains large numbers of
Trigoma Herzogu, young and adult); but Trigonia conocardiformis
is more abundant, and appears to be the characteristic shell here.
Trigona vaw is often found, but it is far scarcer than those just
mentioned ; also Cyprina rugulosa, Astarte Herzogi, and Ostrea.
The middle band, No. 2, Section G, is composed of a fossi-
liferous rock that appears to be, as before alluded to, the equivalent
of the “ Modtola- and Hamites-zone” at McLoughlin’s. At present,
however, I am not aware that any fragments of Hamites africanus
have yet been found in this locality. Only in this bed, and in
Nos. 6 & 7, at McLoughlin’s, is Modiola Bainii found, as far as I
have been able to learn; and the accompanying shells, much like
those found in the corresponding zone shown as No. 7, Section E,
are Ammonites subanceps, Gastrochena dominicalis (in fossil wood),
Alaria coronata?, Cardita nuculoides?, Astarte Pinchiniana ?, and
small specimens of Astarie, Cyprina?, Psammobia ?, Ostrea.
The differences are that, above the Modder Drift, this stratum,
No. 2, is much thicker than No. 7 at McLoughlin’s Bluff, as it here
attains, In some parts, a thickness of 3 feet; the rock also is of a
closer and harder texture, and of a more uniform grey colour, whilst
the black specks of carbonized matter which characterize the
“« Hamites-zone” at McLoughlin’s are, as far as I could observe,
entirely wanting, owing most probably to the sediment of which
this rock is composed having been deposited in deeper water.
This stratum makes its appearance, as 1 have said, at intervals, ~~ _
wherever the mountain-side is sufficiently denuded of the superin-
cumbent soil: thus it is exposed a little above Modder Drift,
again in a kloof (gully) called by Drs. Rubidge & Atherstone, from
the number of Ammonites they found there, “‘ Ammonite Kloof,”
and again some six miles above the Addo Drift, and beyond Com-
mando Kraal on the Sundays River. ‘These indications therefore
enable us to trace this ‘“‘ Modiola-zone” from the bluff, in Section EK,
to the last-named spot, a distance of upwards of fifteen or sixteen
miles. Other indications of this same bed may most probably
be found between these different and widely separated points ;
but the difficulties of making a thorough examination, as I have
previously explained, are very great, covered as many of the hills
are with dense entangled brushwood, while at the same time there
504 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
are few either natural or artifical cuttings through these strata
anywhere.
In the uppermost stratum, No. 1, Section G, I found a number
of Astarte Longlandsiana. In one small mass of rock I obtained
upwards of twenty specimens of different sizes. In a small kloof
near the top of one of the hills, near the Modder Drift, Col. Rocke
and I discovered a place where this fossiliferous bed was exposed,
containing innumerable remains of Pinna Atherstone. I have
never seen such a collection of these shells at any other spot. From
this circumstance we named it “Pinna Kloof.” Tirigona Her-
zogti is also numerous here. If these rocks prove to be, as I sup-
pose, the equivalents of those at McLoughlin’s, there is to be noticed
that, whereas at the latter place the whole series occupies a space of
but some 40 or 50 feet in thickness, here, above the Modder Drift, the
fossiliferous beds are not only thicker themselves, but are separated
by wider spaces of non-fossiliferous rock, it being a height of some
200 or 250 feet from the lowest stratum to the top of “ Pinna
Kloof.”
I was not able to make any satisfactory observation of the dip of
these lower rocks during my visit; but some four or five miles to
the west, on the plateau over which the road passes from the Bay
to Tunbridge’s, I found that the dip of the upper sandstones was at an
angle of 9°, with an apparent direction of 32° E. of 8., taking a
slope from the higher portions of Grass-ridge towards the coast.
These latter rocks, where I obtained this observation, are at a higher
elevation than those examined along the banks of the Sundays
River ; but whether the dip here taken is likely to indicate the true
dip of the lower rocks under notice I am not at present able to
say. A quantity of fossil wood was strewed among the débris of
these strata, although I did not find any in situ; and Dr. Rubidge
informed me that he had found Ammonites in the same locality.
As a recapitulation of the foregoing, I would observe that the
facts here stated, imperfect as they are, and modified as the con-
clusions here arrived at no doubt may be with increased informa-
tion, show that most of the fossiliferous bands in the different
localities of the “Uitenhage Formation” form portions of a series,
and are not continuations of the same zone, as was once thought.
This, I believe, will be proved to be the case, very convincingly, as
soon as their fossils are more accurately tabulated. Thus, in No.
13, at the old road near Rocke’s Bluff, Astarte Bronnii is in very large
numbers, both valves of most of these shells beautifully perfect. This
is the only band from which this Astarte, as far as I can learn, has
been obtained, while I am not aware that a single Trigonia has
ever been found there. In No. 12, Exogyra imbricata is exceed-
ingly numerous; but not one specimen of Astarte Bronniz has been
discovered in it. Here one or two Trigonie make their appearance,
but are very scarce; while in No. 11, near the drift, on the old
road to Grahamstown, Trigonia Herzogii becomes one of the cha-
racteristic shells, In No. 11 also, Cucullea Kraussii, Astarte Her-
STOW—SOUTH-AFRICAN GEOLOGY. 505
zogit, and Pleuromya lutraria are very numerous, these, in fact,
being the predominant forms of this zone. Whether No. 8, in the
kloof near McLoughlin’s Bluff, is a continuation of this (No. 11), as
seems probable, will require further proof. Again, in No. 10, near
Cuyler, Manor, are numerous Ammonites and Trigome, and the
Exogyra of the lower strata has very considerably diminished in
numbers; while in No. 9 we find a perfect ‘“ Trigonia-zone” very
similar to that marked No. 3 in Section G, of the Upper Sundays
River *.
Again, in Section E at McLoughlin’s Bluff, we find No. 7, a
zone containing numerous Hamites and Modiole associated with a
large Ancyloceras(?). This bed seems to have its equivalent in
No. 3, Section G, of the Upper Sundays-River strata; and, lastly, we
have No. 5, inSections E and F, with multitudes of Trigonia ventricosa
and its accompanying Zrigonia vau. To show my meaning better,
I have massed the foregoing Sections A, B, C, E, F & G into one
general one (fig. 3).
B. Saliferous beds of the Uitenhage Formation.—I will now
proceed to notice some sections I have made at the Government and
Bethelsdorp Saltpans, the Koega River, and the Salt Vlei near Port
Elizabeth. These sections represent the stratified clays and sand-
stones of the “ Saliferous deposits” of the “ Uitenhage formation,”
which have been placed by some investigators + as underlying the
Zwartkops fossiliferous sandstones of which we have been speaking.
Government Saltpan between the Zwartkops and Koega Rivers.—The
first locality I shall mention is that of the Government Saltpan be-
tween the Zwartkops and Koega Rivers (see fig. 6, 7, and 7). This sec-
tion (Section I) has been figured and described by Dr. Atherstone +.
1, 2, & 3 are, as he says, thin bands of hard, highly fossiliferous,
dark ferruginous sandstone, about 3 or 4 inches thick, containing
broken shells (Zrigonia, Ostrea, Turritella) and spines of Cida-
vites. These hard bands alternate with saliferous shales and sand-
stones, with a dip of 8° towards the north-east § ; the hard band (1),
overlying porous sandstone, forms the bed of the salt-pan ; and marls
(without salt) and soil cap the uppermost band. It is very difficult
to obtain specimens of the numerous fossils, as they are very perish-
able. Both Mr. Longlands and myself failed, during a somewhat
hurried visit to the locality, to obtain any.
Sandstones on the Koega River.—The sandstones on the banks of
* Mr. G. W. Stow has sent to England specimens of Trigonia Herzogit and
fossil wood with Gastrochene, from the Zambesi, that perfectly resemble in
zoological and lithological characters these fossils from the Sundays River; and
they have their associated Selenite, as at Geelhoutboom.—T. R. J., Oct. 19, 1871.
+ See Dr. Atherstone’s “ Lectures on the Geology of Uitenhage,” Eastern Pro-
vince Monthly Magazine, vol. i. 1857, pp. 581, 584, &., and Quart. Journ. Geol.
Soe. vol. xxiii. pp. 149 & 167.—T. RB. J.
{ See Dr. Atherstone’s sketch section, Hast. Prov. Mag. loc. cit—T.R. J.
§ The beds up the Sundays River (near Geelhouthoom), which Dr. Ather-
stone considers to be equivalent to those of the Saltpan, have a dip, he says
(loc. cit. p. 581), of 8° to the south-west.—T. R. J
506 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
the Koega seem to be very similar in character to those of the
Government Saltpan—so much so that one is almost led to believe
that they must be a continuation of them. Section K (see fig. 6, 6)
was made by me near this river, not far from the old road to Grahams-
town. In this section, No. 1 (at the top) is a marly clay, interspersed
with very numerous, small, caleareous seams. This is comparatively
recent, and rests on a conglomerate of quartzite pebbles (No. 2). Im-
mediately beneath this is clay (No. 3), resting upon a coarse loose
sandstone (No. 4), and this upon a hardened clay.
Two or three miles lower down the Koega, where I obtained
another section, the sandstones appear to be very similar, in their
lithological character, to those shown in the section (Section L) of the
upper rocks at the Bethelsdorp Saltpan (see fig. 6,4). I have not found
any fossils in them, nor have I heard of any being found; we
must therefore look for some further proofs before a positive
opinion of their identity can be formed. ‘This last-mentioned sec-
tion on the Koega is capped with the same Posttertiary shell-lime-
stone as at the Zwartkops.
Bethelsdorp Saltpan.—On the west side of the Bethelsdorp Salt-
pan is a very good section of the saliferous clays and sandstones.
Commencing from the lowest in Section M1 & M 2 (see fig. 6,5), No. 22
is a coarse, gritty, rather loose sandstone, the thickness of which is
at present unknown, as is also the thickness of the belt of clay
(No. 21) resting upon it. It is highly probable, however, that the
latter, if properly exposed, would prove to be banded clay and sand-
stone, some 2 or’ 3 feet thick, similar to Nos. lida, 17, and 19.
No. 20 is a hard, compact, fossiliferous sandstone, not more than
1 foot thick. In this the characteristic fossils of the locality are
found, namely the remains of Cidaris pustulifera. Its plates and
spines are obtained here in large quantities. Judging from the
numerous remains, one is led to the belief that it was during the
period of the deposition of this particular zone that it most flourished,
while at the Government Saltpan these fossils appear scarce. Ostrea
Jonesiana is also frequent in this belt, whilst other small Ostree
are scarce. Dr. Rubidge found Crassatella complicata here. Above
this fossiliferous bed we find fifteen alternate bands (altogether
10 feet 9 inches) of a reddish clay and sandstone (stratum 19),
each bed being very distinctly marked. These bands seem to be
non-fossiliferous, as well as the other strata from No. 19 to 14
in; Section M 1 & 2, and from No. 11 to 8 in Section L. More
diligent search, however, may discover traces of life not only in
these rocks, but also in the upper strata before alluded to, on the banks
of the Koega (Sect. K, fig. 6,6). Above No. 19 in Section M 1 & 2,
is a coarse non-fossiliferous sandstone (No. 18), 8 feet thick ; then
follow banded clays and sandstones (No. 17) 3 feet 6 inches; and
above these, 4 feet 8 inches of sandstone (No. 16); again alternate
bands of clay and sandstone (No. 15a), 5 feet 3 inches thick; then
2 feet of a light-coloured friable sandstone (No. 156), on this a
band of 8 inches of clay (No. 15c), and above that 4 feet 4 inches
of a light-coloured and very friable sandstone (No. 14). On the top
STOW—SOUTH-AFRICAN GEOLOGY. 507
of all these lies an irregular deposit of a sandy calcareous tufa,
covered with a reddish sandy clay. The remarkably uniform thick-
ness of the several clays and sandstones in these sections is worthy
of notice.
From another Section, marked L (see fig. 6), that I was able to ob-
tain in a higher bank about 300 or 400 yards to the N.N.E. of
Section M 1, No. 14 does not appear to be the uppermost in this
series. This higher section shows nearly the same dip as the lower
one; and in it we find a broad band of sandy clay (No. 11) 8 feet
in thickness, interspersed with a great number of calcareous stripes
near the top. Above this is 2 feet of clay (No. 10) of a pale-greyish
stone-colour, (No. 9) six inches of a sandy yellow and brownish
striped clay ; and above that, (No. 8) two feet more of the same clay
as No. 10, with a superficial loam. In the foregoing sections,
we therefore obtain Gif the uppermost bands belong to the series)
a combined thickness of more than 52 feet of these stratified clays.
The latter section is capped with the same reddish sandy clay as the
former ; and I have not been able to find in these two places any
trace of a deposit that might be considered the equivalent of the
Zwartkops and Koega Posttertiary shell-limestone.
The Salt Vler near Port Elizabeth.—Ahbout five miles nearer to
Port Elizabeth, in the clay-pits, at a place called Salt Vlei, we find
another excellent section of the stratified clays. This is shown in
Section N (fig. 6,2). In these pits the lowest uncovered rock is that
marked No. 18 in the section—namely, a marly, gritty sandstone.
It is exposed for a depth of 14 feet; the remainder of it (whatever
the entire thickness may be) is covered up with the débris of the
excavation. It appears, as far as can yet be seen, to be non-fossili-
ferous. Immediately above this is a belt of clay (No. 17), and on
the clay a band of nodular concretions (No. 16) fourteen inches thick.
These nodules are irregular in shape, and of various sizes, some of
them being upwards of 2 feet in length; when broken they all
display the same fracture as that shown in specimen No. 16*, witha
powdery nucleus as in specimen No. 16ay. Jn siti, they lie as if
they had been regularly packed, their greatest length being in the
direction of the dip.
Above this noduliferous band is a sandy clay, No. 15, 2 feet
thick, of a yellow-ochre colour. Upon this follows a dark slate-
coloured clay, No. 14, also 2 feet thick. The strata Nos. 14,12, and
10 are clays to all appearance exactly alike, as regards colour and
texture, and must have been deposited under similar circumstances.
No. 13, 1 foot thick, is the first zone (in this section) in which were
found traces of fossils. It is full of small marine shells [_Astarte (?)
and Natica or Phasianella (?), T. R. J.]: some are very beautiful ;
and all were so delicate in structure as to be very difficult to remove.
No. 12 is a clay, 3 feet thick; then comes a single line of
nodules, No. 11. These nodules are placed either singly or in groups,
as shown in the section, all in the same line of bedding. No. 10 ig
* No. 16. Ferruginous sandy nodule, with ochreous centre.—T. R. J.
+ No. 16a. Dark red-purple earthy hematite.—T. R. J.
508 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. =
a clay, 73 feet thick. No. 9 is
an indurated shell-band, 3 inches
thick ; its shells are different from
those found in No. 13. Some of
the species that make their first
appearance here go on increasing
in numbers in the deposits marked
8and 7. Specimens 9, 9a, 9b, con-
tain numerous fragments and casts
of shells, obscure gregarious bi-
valves [possibly Cyrena, T. R. J.].
No. 8 is a clay, from 18 inches
to 2 feet where thickest, inter-
spersed with streaky patches of
shells [ Cerithiwm ?, T. R. J.], the
intervening clay being devoid of
them.
No. 7 is a deep-red clay, with
yellow stripes running through it.
This, like the preceding, has bands
of shells (small bivalves and uni-
valves).
It is remarkable of these three
last-mentioned strata, -Nos. 7, 8,
and 9 [which may be of estuarine
origin, T. R. J.J], that they gra-
dually thin out.
The deposit No. 6 is a light
slate-coloured clay, 9 feet 2 inches
thick. No.5 is a narrow band of
clay, varying in width from 1 to
3 inches, full of fragments of shells,
with a small Ostrea in abundance.
Above this is a deposit of a similar
light slate-coloured clay, Ne. 4,
8 feet 6 inches thick ; and upon
this a stripe of a yellowish sandy
clay (No. 3) or, rather, a loam,
pulverizing between the fingers;
and above it is a clay similar to
Nos. 4 & 6, two feet thick. This
is capped with a sandy kind of
marl, No. 1,varying from 2 to 4feet
(Section O of Author.)
h. Adolian sandhills,
The F
d. Limestone and sandstone (see fig. 5).
ce. Stratified clays.
g. Red clay (superficial).
b. Caleareous tufa.
f. Posttertiary limestone or shell-bank.
a'. Loose shingle in soil.
Salt Vlei.
* The sides of this outlier were too
thickly covered with débris for me to
obtain a good section; but I imagine
that it must be similar to the stratified
clays at the Bethelsdorp Saltpan, as the
spines of Cidaris pustulifera are found
in the débris.
Fig. 4.—Seetion of the Salt Vlei and Flat, on the South Side of the Creek or Ferreira’s River.
e. Clays and sandstone *.
——
CEEAPGLLUS
e (\
a. Quartzite hills of Port Elizabeth.
AGE EGE
x BLYF
KHOA
WwW
Zi
Ay
4
STOW—SOUTH-AFRICAN GEOLOGY. 509
thick, interspersed with calcareous stripes. From this stratum (No.
1) small burrows or pipes have been sunk through the strata Nos.
2&3, and form cavities in No.4, as delineated in Section N.
Some of these curious excavations are several feet in depth; and in
some instances the lower part is 18 inches wide, while the pipes
leading to them are only a few inches in width; they appear to be
the work of some of the old inhabitants of that ancient sea. They
are now all filled with the sandy marl of No. 1, with which are
mixed small nodules, and, in some of the pipes, fragments of shells,
evidently all washed in from above, when the apertures leading to
them were open.
These clays dip E. by 8S. at an angle of 20°, and have been denuded,
as shown in the Section. The sandy marl and the outcrop of the
clays are covered with surface-soil, the lower part of which is inter-
spersed with beds of well-worn quartzite pebbles, in some parts to a
thickness of from 1 to 3 feet. In some places thereis a small deposit
of calcareous tufa between the underlying clays and the surface-soil.
In another excavation, near the same spot, I obtained a rather
different section of these stratified clays exposed for about 39 feet,
as seen at c,in Section O (fig. 4). The dip here varied from 10°
to 20°. Whether the clays of these two last-mentioned Sections (N
Fig. 5.—Section of the beds marked d in Fig. 4*. (Section P of
Author.) From an excavation made for a large tank.
Soil and pebbles.
Tufa, 12-18 inches.
Wi! Rather friable sandstone, interspersed with carbonate of lime, 2 feet.
Tufaceous limestone, 5-7 inches.
Sandstone, interspersed with carbonate of lime, 13 inches.
b Tufaceous limestone, 1 foot.
_ Sandstone, 3 feet.
Sandy limestone, 6 inches.
Sandstone, 7 inches.
; \ Sandy limestone, 6 inches.
Sandstone, 1 foot.
Reddish sandstone.
Bottom of excavation.
and O) are continued across the Salt Vlei to the opposite outlier d in
Section O (fig. 4), I am not able to say, as the sides of this hill are
_* Possibly this section includes some Posttertiary deposits.
510 PROCERDINGS OF THE GEOLOGICAL SOCIETY.
too thickly covered with soil &c. to obtain a trustworthy section ;
nor can I, of course, say whether its strata assimilate rather to the
clays and sandstones of the Bethelsdorp Saltpan; but Dr. Rubidge
told me that he picked up a number of the spines and plates of Cidaris
pustulifera among the débris of this outlier. All I can speak of
with certainty is from Section P (fig. 5), which I was able to make
during the excavation of a large tank on the top of this outlier. In
this section the surface-soil was interspersed with shingle (as in
Section N). Below this was a band of tufa, from 12 to 18 inches in
depth ; then 2 feet of friable sandstone, interspersed with carbonate
of lime, as shown in the section ; again tufaceous limestone, from 5
to 7 inches; beneath that, 13 inches of sandstone, interspersed with
carbonate of lime in the same manner as the sandstone above; again
1 foot of limestone, then sandstone 3 feet; below this, three uneven
belts of sandy limestone and sandstone, respectively 6, 7, & 6 inches
thick ; these were followed by 1 foot of sandstone, of the same cha-
racter as the thick band above; and beneath them all, at the bottom
of the excavation, was a reddish sandstone, the thickness of which is
at present unknown.
Very little is accurately known of the fossil contents of the strata
shown in the last three sections. They evidently require attentive
examination, and promise a rich harvest to future explorers. Since
my departure from Port Elizabeth, Messrs. Kemsley & Burness have
found fossil Ferns in some of these clays, but have not been able to
identify them with any of those from Geelhoutboom, on the Sundays
River*. The clay in which they were found <<‘ rested upon sandstone
containing immense fragments of leaflets and petioles of Zamie,
mixed with pieces of wood.” ‘To this discovery I shall have to allude
again (p. 513).
Résumé of the Strata of the Saliferous Growp.—None of these
sandstones that I have examined possess the close, compact nature
of those found among the rocks of the Lower Twartkops in Section
A (fig. 3) ; but they are all of a coarse gritty texture, very like those
I have spoken of as being found on the Koega (p. 506).
In looking over the various sections of these stratified clays and
saliferous sandstones (namely I—P), one cannot help being impressed
with their diversified aspect, each section differing widely from the
others; and they seem to indicate that we are not examining a
single wide-spread deposit, but a partially consecutive serzes, some-
thing similar to, but of more limited extent than, those of the
Uitenhage formation before considered. This becomes more appa-
rent by looking at the diagram (fig. 6), in which the foregoing sec-
tions are collated and compared.
Here the section near the Salt Vlei, noticed by Messrs. Kemsley and
Burness (fig. 6, 3), becomes an important addition, as by it we find that
Trigone, Turritelle and a Gervillia were obtained from the lowest
stratum of sandstone in this formation, while the clays with Ostrea
and Tellina (?) are above. This sandstone deposit appears to be one of
the oldest, if not the most ancient, of this Saliferous formation,
* Quart. Journ. Geol. Soc. vol. xxiii. p. 145 &e,
Sandstones and Limestones.
1. Outlier near
the Salt Viet
(Sects. O, P,
figs. 4 & 5).
Sandstones and Clays.
[Zo face p. 510,
idiferous Group.
7. Government
Saltpan
(Sect. I).
Tufa. Post-
tertiary.
Shale and
Sandstone.
22
Shale and
Sandstone.
3
Sandstone.
Dip 8° to N.E.
1, 2, 3. Hard, highly fossiliferous bands, with Cidaris pustu-
hfera, Ostrea Jonesiana, Trigonia, Turritella (?).
&
Sandstones and Limestones,
Fig. 6.—Collated Sections, showing the probable succession of the Clays
2. The Salt Vlei
near Port Hlizabeth
(Sect. N).
1, Outlier near
the Salt Vlei
(Sects. O, P,
figs. 4 & 5).
Clay with Ostrea.
}
thium (?), &e.
11 Nodules.
12
13 Clay with Astarte, &e.
14
Sandstones and Clays.
15
=| 14 Nodules.
7
18
Dip 20° to E. by S.
Spines of Cidarzs
pustulifera in
débris.
Estuarine beds with
Cyrena (2), Ceri-
(Section Q of Author, embracing his Sections I, K, L, M,
3. Near the Salt 4. Near 5. Baise? oo
Vlei (Kemsley Ger nD. (Sect. KC),
and Burness)
(Sect, 8).
5
Se.
Dip 6° to N.E.
Clays and Sandstones,
Cidaris and
Ostrea.
Dip 6° to N.E.
Clay with Ferns.
Sandstone with Zamia and wood.
{Clay with Teliina, Pleuromya,
Ostrea, &e.
‘ner Sandstone, with Twrri-
tella Rubidgeana (common),
Trigonia Herzogii, T. Gold-
| fussi, and Gervillia.
}
and Sandstones of the Saliferous Group.
N, O, and S.)
t
'
'
[Zo face p, 510,
}
7. Government
Saltpan
(Sect. I),
1 Clay and Tufa. ) Post.
2 Pebbles. tertiary.
3 Clay.
-) 4 Sandstone,
Z, > Clay.
St cc
Marl
Shale and
Sandstone.
2
Shale and
Sandstone.
: 3
Sandstone.
Dip 8° to N.B.
1, 2, 3, Hard, highly fossiliferous bands, with Cidarie pustu-
lifera, Ostrea Jonesiana, Trigonia, Turritella(?).
STOW—S80UTH-AFRICAN GEOLOGY. 511
The strata of the Government Saltpan seem to follow, with (accord-
ing to Dr. Atherstone) Trigonia, Turritella, Ostrea, and Cidaris
pustulifera. At the Bethelsdorp pan C. pustulifera is found in the
greatest abundance; and spines and plates of the same Cidaris,
found scattered on the sides of the outlier at the Salt Vlei, near
Port Elizabeth, indicate the position of the associated clays on the
opposite side of the Vlei (Section O, fig. 4), with their innumerable
specimens of small Ostrea unmixed, as it seems at present, with
the remains of Cidaris. As I have already said, so little is yet ac-
eurately known of the fossil contents of all these different strata
that nothing can be done to decide the question of position with any
degree of certainty until the fossils shall have been more fully
studied and classified.
On looking at these collated sections (fig. 6) we at once see how
much they differ from the apparent uniformity of the sandstones of
the Zwartkops and Sundays Rivers (Sctions A-G, fig. 3). These
latter exhibit the features of an extended and uniform deposit, while
the former display local differences of a very diversified character.
Further, the more I have studied them the more I have been im-
pressed with the idea that the position at present assigned to them *
is not correct.
The following reasons may be given to explain this opinion. It
is said that these strata are an earlier formation than those of
the Zwartkops and Sundays Rivers series; but has this been con-
vincingly proved? As far as I could obtain information, no good
section has yet been pointed out (that is, anywhere between the
quartzite hills of Port Elizabeth and the Grass-ridge) where these
clays &c. are so situated as to demonstrate distinctly that they are
really below, and the Zwartkops Trigonia-beds above. Even should
we find them in a depression apparently lower, still this would prove
nothing without a satisfactory junction in which the Trigonia-beds
could be shown to be placed above the stratified clays; whereas
sections have been found the reverse of this. It might as well be
argued that the red clay (g, g, in Section O, fig. 4) spread over the
surface in different parts of the Oliphants-Hoek and Port-Elizabeth
Divisions, instead of one of the most recent clays, is a very ancient one,
because in the former locality it has been found (in sinking wells)
to be upwards of 100 feet in depth, and in the latter, near the New
Prison, about 70 feet—lower levels than either the sandstones or
stratified clays have been found at. This clay has evidently been
deposited in hollows, eroded out of the more ancient rocks; and in
the same way, I cannot help thinking, these “Saliferous Strata”
have been deposited in positions where denudation had removed
some of the earlier formations. This was especially the case where I
examined the strata of the Government Saltpan ; for there these rocks,
as far as I could judge, when the dip of the Yrigonia-sandstones is
taken into consideration, must be placed above those of the Zwart-
* That is, delow the great Trigonia- and Ammonites-series of the Uitenhage
formation. See Atherstone, doc. cit., and Quart. Journ. Geol. Soc. vol, xxiii. p.
149,—T, R. J.
512 PROCEEDINGS OF THE GEOLOGICAL SOCTETY.
kops. Again, as a proof that their position is below the Zwartkops
Trigonia-beds, it has been stated that these saliferous rocks are found
resting unconformably on the quartzite and clay-slate, in the direc-
tion of Bethelsdorp and Chatty. But, again, this of itself is no proof ;
for near the Shark’s River one of the most recent shell-deposits
also rests directly on the quartzite.
Dip.—We will therefore first enter into the question of dip,
especially that of the Government Saltpan—in the first place, how-
ever, premising that between this Pan and the saliferous deposits of
Bethelsdorp and the neighbourhood of Port Elizabeth the strata of
the Zwartkops, as shown in sections B&C intervene. The Pan
itself is in a denuded depression ; but this hollow is not very deep,
as is indicated by the rising ground that surrounds it, and from
the top of which a plateau stretches on the same level as the upper
edge of the Zwartkops Heights—in fact, is continuous with them,
as is seen at d’ in Section R (fig. 7).
Dr. Atherstone * says that the strata at Geelhoutboom dip 8.W..,
towards the centre of the ancient estuary, at an agle of 8°, and those
of the Zwartkops conversely N.E.; and he gives the dip of the Salt-
pan rocks at the same angle to the north-east, that is, in the same
direction as those of the Zwartkops. Now it is certain that for a
number of miles together the dip of the Zwartkops strata continues
with great uniformity at nearly the same angle. But an angle of
8° gives a depression of about 1 foot in 15; and if continued two
miles (about the distance of the Government Saltpan from the top
of the Zwartkops Heights), there would be a total fall of some 1500
feet. The highest hills anywhere in the neighbourhood are the
Koega Kopjes; and they are only 480 feet above the level of the
sea. The depression of the Saltpan is certainly not 300 feet below
the level ef the Amsterdam Flats, the plateau from which these
Kopjes rise, as that would place it below the level of the sea, which
it decidedly is not; but, even allowing it to be so, the angle given
would place the Zwartkops sandstones, if they extended as far as the
saliferous strata of the Saltpan (which I think is not doubted),
1200 feet below them. A dip of 4° (the same as at Rocke’s Bluff)
would allow rather more than 700, or some 400 feet below: and
even the small angle of 2° would still leave the Trzgonza-beds be-
tween 70 and 80 feet lower than the deposits of which I am
speaking.
Fossils.—At the Government Saltpan (p. 505) Dr. Atherstone has
found Trigone and Turritelle associated with Ostree and Cidaris
pustulifera. I cannot help thinking that this is the oldest portion
of the saliferous strata that has been yet examined. The stratified
clays of the Bethelsdorp Pan and those at the Salt Vlei are, I be-
lieve, more recent. At the former of these Cidaris and Ostrea
are abundant; but no Tirigonie are yet known there; while at the
latter spot no specimens of either the one or the other have been ob-
tained, although Cidaris has been found on the sides of the outlier
(Section O, fig. 4) on the east of the Vlei. This outlier, I believe,
* Loe. cit. p. 581, and woodcut, no, 1.
STOW—SOUTH-AFRICAN GEOLOGY, 513
will prove to be older than the clays of the Salt-Vlei section, and
probably equivalent to those of Bethelsdorp.
At one of the meetings of the Natural~History Society of Port Eliza-
beth, Dr. Rubidge published a section (Section §, fig.6,3), near the Salt
Vlei (see a notice of their Proceedings in the ‘ Port-Elizabeth Tele-
graph’), at the top of which is a bed of clay, “No. 1, apparently about
one foot.” This is the stratum in which Messrs. Kemsley and Burness
discovered the Ferns (see above, p.510). ‘The stratum of clay which
contained the Ferns rested on a sandstone containing immense frag-
ments of leaflets and petioles of Zamie, mixed with pieces of wood,
and that on aclay with shells (ellina, Orbicula [?], Myacites [ Pleu-
romya|, Ostrea, &c.); no 2, some three feet thick. Below this was
a shelly sandstone, containing Turritella Rubidgeana (Tate), with
imperfect specimens of Trigonia Goldfussi, and a new species of
Gervillia. The discovery of these shells, which are on the oppo-
site hill (near Mr. Graham’s house) associated with Cidaris pustu-
lifera (Tate), at the Bethelsdorp Saltpan with the same and with
Crassatella complicata (Tate), Ostrea Jonestt (Tate), and at the Zwart-
kops Heights with Trigoniw, Astarie, &e., is of great interest, as
showing clearly the relation of the whole series of the beds of the
ancient Mesozoic bay to each other.”
I wrote to the late Dr. Rubidge upon this subject immediately
after the publication of the report, to ask him his opinion whether
this did not confirm the conclusion I had already arrived at from
the study of the dip. Unfortunately I did not receive an answer.
Distribution of Fossils in the several members of the Uitenhage Forma-
tion, according to the corrected lists of named species—T. R. J.
Speciea
Species ~ |Community of species
yielded. es between
1. Near the mouth of Sun- ( 28 12 1&2 =12?
7 days River............... 62?
2. ee up Sundays Ri- | | 46 | 99 ne Tee
Tl.|Zwartkops River ............... 28 9 WT. with Il. &IIl= 6?
“ Lowest strata of the Fin eyed
we { Zwartkops Crag (cuit | ae 9 Ho IV
TY.|Saliferous strata.................- 9? 3 1. &.= 0
Ii. & 1IV.= 0
EVE wie
C. Conclusion.—Let us now take a retrospect of the various fossili-
ferous beds I have mentioned. In the lowest Zwartkops stratum no
Trigonice, as far as I can learn, have been discovered, and certainly
not the Crassatella complicata, Hamites, and some other shells. As
we proceed upwards Trigonie become abundant, and increase in
number of species. Ammonites also become frequent in some strata.
At M‘Loughlin’s Bluff on the Sundays River Hamites africanus,
VOL, XXVII.—PART I. 2N
514 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Crassatella complicata, and Trigonia Goldfussi make their appearance.
These rocks, it will be remembered, I have looked upon as the upper-
most of the Zwartkops- and Sundays- River strata. At the Government
Saltpan, Trigonie and Turritelle are mixed with the remains of Cida-
vis—while in the section near the Salt Vlei (Sect. 8, fig. 6, 3) we find
Crassatella complicata and T. Goldfussi, together with a Gervilla
(shells found in the wppermost Sundays-River strata), imbedded in
a sandstone, immediately above which are found stratified clays con-
taining shells which, together with Crassatella complicata, are asso-
ciated with Cidaris pustulifera, the characteristic shell of the fossi-
liferous zones of the Saliferous Strata, and, apparently, the Trigome,
Ammonites, and their associates are absent. This explanation proves,
I think, the regular sequence of the shells.
Mr. Tate, in his paper “ On some Secondary Fossils from South
Africa,” says*:—‘ Species of this type (Cidaris pustulifera) exist
at the present time, and are found in the Tertiary and Creta-
ceous rocks; species of the type with crenulated bosses characterize
Oolitic deposits. There are, however, some exceptions to these rules,
and for the present the African species may be regarded as another
exceptional example.” If I understand this rightly, some species
of Cidaris (this fossil, remember, is associated with Orassatella
complicata) are indicative of Cretaceous rocks; but this is an “ ex-
ceptional case.” If, then, these same deposits are placed in the
position which I believe is their true one, the exceptional condition
vanishes; they take their right place, and prove that the law which
regulated, with regard to periods, the development of particular
races was the same in the southern as in the northern hemisphere.
Origin of the Salt.—The author thinks that the Trigonia-series, hay-
ing been deposited in open sea, would be less likely to contain salt than
shallow-water beds succeeding them and formed in narrowing creeks
and lagoons. ‘The saliferous series he believes to have thus suc-
ceeded the Zrigonia-beds, and to have become impregnated with
salt. At the present time the same causes are at work on a smaller
scale, in the mouths of some of the mimor rivers of South Africa, where
the entrances are blocked up with sand and thus communication with
the ocean is cut off, except when broken through occasionally by a
freshet after heavy rains. During the time that these mouths are thus
land-locked the evaporation is more rapid than the supply ; and as a
natural consequence, the water in the enclosed basins becomes more
intensely salt than that of the neighbouring sea. The deposits formed
within them are saturated with this extra-saline fluid, so that when
a flood bursts through the opposing barrier, and the water of the
imprisoned river falls with the tide, banks of brackish mud are ex-
posed in many places; and these soon prove themselves to be salife-
rous deposits ; for, as they dry in the sun, they become covered with
a white saline efflorescence. Such, one cannot help believing, is
the explanation of the mode of formation, although on a grander
seale, of the saliferous strata we haye been considering.
* Quart. Journ. Geol. Soc. vol. xxiii. p. 163.
STOW—SOUTH-AFRICAN GEOLOGY.
Parr I, § 2, Terttary or Postrertiary Strata.
[Abridged*.]
1. Pliocene or Postpliocene Strata
of the Interior.—Having thus no-
ticed the older rocks, I will now
proceed to make a few remarks
on the so-called “ Tertiary Lime-
stone”?, which covers in many
places the rocks we have been
describing. This series caps the top
of the Zwartkops Cliffs, extend-
ing from Rocke’s Bluff (see Sec-
tion R, fig. 7), along the top of the
hills towards Uitenhage, and rest-
ing upon the Jurassic sandstones.
The greatest accumulation appears
to be on the Amsterdam Flats and
the Grassridge. At the Koega it
is found upon the friable non-
fossiliferous sandstones of that
locality (see above, p. 506). At
the Sundays River it is seen on
MeLoughlin’s Bluff as a narrow
belt. ‘These positions are shown
in Sections E and R (see fig. 7).
From the Zwartkops to the quart-
zite ridges of Port Elizabeth, I
am not aware that any traces of
it have been found. Mr. Pinchin,
who has paid much attention to
this formation, states (in a letter)
that “it covers the upper part
of the plain (Amsterdam Flats),
extending westward to Hitzeroth’s
(the Old Government) Saltpan,
and along the tops of the hills to
within a mile of Uitenhage ; it
covers the whole of the Grassridge
* The sections and sketches sent by
the Author for this portion of his Me-
moir are deposited with the others in
the Society's Archives; and the large
collection of recent and fossil shells &c.
sent by Mr. Stow, in illustration of his
views as given in this paper, awaits ex-
amination by Mr. W. S. Dallas, who
kindly promises a full report.—T. R. J.
+ This is the limestone termed “ Ter-
tiary’’ in Mr. Bain’s Geological Map
of the Cape Colony, Geol. Trans, 2 ser.
vol, yii. pl. 20.—T. R. J.
2n 2
and Positertiary Shell-Limestone.
Fig. 7.—Section showing the relative positions of the Trigonia-beds, the Saliferous group,
(Section R of Author.) Length about 25 miles,
McLouehlin’s
Bluff.
Sundays
iver.
Grassridge.
ga
ver.
4
Koe
ga,
opjes
(480feet). BR
Koe
K
Government Saltpan.
Zwartkops Rocke’s
Bluff.
River.
Amsterdam Flats.
515
d, d'. Posttertiary Shell-beds.
¢. Soft friable Sandstones.
b. Saliferous beds.
a, a. Zwartkops- and Sundays-River Sandstones.
516 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
to within three miles of Prentice Kraal, and nearly in the same meri-
dian as Blaaw Krantz. This latter place, however, is some three or
four miles off the limestone. It is seen upon Landman’s Kop, a
hill lying just eastward of the Sundays River’s mouth, and at Deep
Kloof and Groof Water, in Oliphant’s Hoek, twenty miles south of
the Sundays River. To the southward of Port Elizabeth the lime-
stone hills of Buffel’s Vontein, Chelsea, and Van Staden’s River, are
probably of the same formation.” als:
Mr. Pinchin’s professional duties have given him opportunities of
visiting every part of the district. The places which I have ex-
amined are :—Rocke’s Bluff; a quarry on the flat between the Go-
vernment Saltpan and the Zwartkops Heights ; on the banks of that
river, to a deep kloof, a little below the drift (ford) on the old
Grahamstown Road; the old waggon-track on the north bank of
the Koega, near the Kopjes; different spots on the Grassridge ;
and at McLoughlin’s Bluff. It seems to be a single deposit, and
not a series like the others (see p. 519). It varies very little
in all the localities that I visited, being from 4 to 6 feet thick,
except at McLoughlin’s Bluff, where it is much thinner. It is
highly fossiliferous, and abounds with fragments of shells, and
now and then with some that are nearly perfect. Of the bi-
valves only single valves are found, and the majority have been
broken by the action of the waves. In some localities there are
immense deposits of a large species of Ostrea. Out of 22 dif-
ferent species of shells, nine are not at present found on the neigh-
bouring coast, five are still doubtful, leaving only eight of the
number that are positively recognized as being inhabitants of the
present sea. rene
2. Pliocene or Postpliocene Strata on the Coast.—Following this lime-
stone, and with an evidently wide interval, is a series of deposits
which are spread out from Port Elizabeth to the mouth of the creek (or
Ferreira’s River), and thence, in detached spots, to the Zwartkops.
The oldest deposit appears to be a sandy tufaceous (?) limestone,
interspersed with many patches of conglomerate, formed of small
quartzite pebbles. It is very fossiliferous. Out of twenty-five
species of shells that I collected from this bed, twelve have not been
found in the adjoining sea. The: greater portion of these are frag-
ments. This deposit was certainly laid down under widely different
circumstances from those of which I shall have to speak presently,
and in which the shells, however fragile and delicate, are in a
beautifully perfect state.
As far as I could judge from an excavation I had made at the
foot of the cliff, I found this stratum to be from four to eight feet
thick; but I found great difficulty in obtaining a good section, as,
at the lowest level arrived at, the water flowed in so rapidly that we
could not proceed. The bed extended from a quarter to half a mile
inland, where it was hidden under the eolian sandhills. It was
covered by a non-fossiliferous limestone, a few inches thick; and
above that was spread a layer of loose pebbles of the same kind as
those in the pebbly limestone itself.
STOW—SOUTH-AFRICAN GEOLOGY. 517
In two other diggings, instead of the loose shingle, occurs a clayey
sand, mixed with small pebbles and numerous shells (Cerithium &c.),
out of twelve species of which, seven have not yet been found on the
present beach. Most of the shells are broken and worn, owing no
doubt to their having been rolled in shallow water with the sand
and small shingle in which they are imbedded.
Further south, after digging in a bed representing that last described
for about eighteen inches, the influx of spring water prevented the
examination being carried further. Above it was a hard limestone
without fossils, and above this a band of pale slate-coloured sand
from 9 to 18 inches thick, equivalent to the pebbly clayey sand
above mentioned. It is mixed with grit and small pebbles, and
contains numerous specimens of the straight Cerithiwm which occurs
in the equivalent bed; but all the shells found in it are broken and
waterworn. Near the Creek there is a bluish sand ; and the shells
in it are more perfect than in the beds previously mentioned. I had
no opportunity of obtaining a measurement of its greatest thickness.
From this particular band I have collected forty species of shells, of
which there are eighteen that have no living representatives on the
present sea-beach. I imagine that their descendants will have to be
looked for further to the eastward along the coast.
There are two strata in the southern part of the section whose
equivalents I have not been able to trace further north. One isa
bright yellow sand, from 1 to 2 feet thick, containing numerous per-
fect specimens of Loripes edentula (Chenu) and Mactra, with both
valves complete. The other is a pale slate-coloured sand, slightly
clayey, varying from 2 to 5 feet in thickness, and containing numerous
beautifully perfect shells. From the immense numbers of the
Akere found in it, I have termed it the Akera-stratum. This deposit
is in some places worn away, and divided in detached portions, as
represented at a,a,ain Section T. It is at many places capped
with a layer of waterworn fragments of shell-limestone, pieces
of shell-grit containing small pebbles, and also waterworn shells of
the present ocean. These last were, of course, left in the position in
which they are found during the retreat of the sea to its present level.
The number of species of shells that I have already obtained from
this stratum is 71 ; of these, 27 have not been found on the present
coast, and of 10 others it is doubtful whether they are still living
in the neighbouring bay. The straight Cerithium, the Pectunculus,
and others have sometimes been picked up by shell-collectors on
the beach, mixed with recent shells; but, possessing none of the
fresh appearance of more recent shells, they have always borne
evidence of haying been disinterred.
§ 3. Pliocene or Postpliocene Strata (Raised Beaches) on the Coast
and Inland.—The next deposits, so far as at present known, in suc-
cession to these, are shell-banks that are not only found along
the coast, forming a raised sea-beach, as on the south side of the
Zwartkops River’s mouth, but also extending inland as raised banks
nearly as far as Cradocktown. ‘They are evidently far more exten-
sive than those we have just been considering. The principal parts
518 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
that I have examined are:—the raised beach just mentioned, which is
about half a mile from the river’s mouth, and 40 or 50 feet above
the present sea-level; on the south bank of the Zwartkops, near
Rawson’s Bridge; and along the banks of the creek and Ferreira’s
River, towards Cradocktown. No trace of these shell-beds is found
on the surrounding highlands.
This formation is also found protruding through the red clay that
forms a portion of the flat, between the outlier marked No. 1 in the
section (fig. 4) near the Salt Vlei and the sandstone on the coast
near Port Elizabeth. See fand gg in that section (p. 508).
In each locality mentioned this deposit extends a considerable
distance. Thus it can be traced from a spot where it is exposed by
a cutting through the north bank of the creek, on the Grahamstown
Road, across the raised flat over which the road passes towards the
Zwartkops, until you reach the wide alluvial flats that extend from
the south side of the river. Again it stretches from the road men-
tioned to the sand-hills along the coast. This portion, however, is
covered with soil, thickly interspersed with shingle, mainly composed
of pebbles of quartzite, from the distant hills. Wherever any wild
animal has burrowed through the soil and shingle, or where any
excavation has been made, the shells of this deposit are almost in-
variably exposed to view. In like manner it evidently extends
towards Port Elizabeth—as it there again makes its appearance, as
indicated in the section alluded to (fig. 4). We must note that we
have here the shingly beds with the red clay superposed ; I shall have
again to refer to the last-named deposit.
I have found the shells from these ancient shell-banks on the
coast near the mouth of the creek, evidently washed out and spread
over the surface.
Returning to our first point of departure, we can trace the shell-
bed, exposed at intervals, along the banks of the creek and Ferreira’s
River, towards Cradocktown, as before mentioned; and, after passing
the mud-flats on the south side of the Zwartkops River, we find it
again, extending along the banks of the same for more than half a
mile. In this locality it was evidently at one time of much greater
extent than at present, and must have occupied the very course of
the present river; but it is being rapidly worn away by the action
of the stream.
In some parts (at the bridge) this deposit is nearly 30 feet thick.
It is composed principally of sand, the upper portion being inter-
laminated with bands of limestone. This is especially the case at
the western (or what was its mland and most sheltered) extremity.
In these bands are imbedded large quantities of shells. At this
spot a large and characteristic Panopea is found. It is generally
buried in the lower part of the stratum, and rather frequently with
both valves entire. This is the only bank in which I have found
this shell, with the exception of a solitary specimen in the raised
beach before mentioned. At the creek and the banks of Ferreira’s
River, I have not found any indications of it. At this place (Rawson’s
Bridge) a large Solen is also very plentiful, as well as a Mactra and
STOW—SOUTH-AFRICAN GEOLOGY. 519
a Tapes ; these shells are perfect ; but, although they are so numerous,
many of the shells found in the banks at the creek and Ferreira’s
River are wanting. It is worth considering whether or not this in-
dicates a series of these deposits. All the shells in the lowest part
of the stratum at this spot have both valves perfect, some of the
Mactre still retaining a portion of their colour; those imbedded in
the limestone, nearer the surface, are in a more fragmentary con-
dition.
The section I have called “the raised-beach” is, as above stated,
some 40 or 50 feet above the level of the sea; but unfortunately the
upper portion is the only part sufficiently exposed for examination.
From the indications on the beach below, it most probably rests on
a sandstone there shown. Almost every shell in the remains of
this ancient beach is broken, in the same manner as those now
found on the present sea-shore where exposed to the full action of
the waves rolling in from the ocean.
At the creek on the Grahamstown Road this deposit has been
cut through for some 12 feet in depth. Here, again, most of the shells
are perfect, and do not seem to have been exposed to the action
of rough water. This is eminently the case with the contents of the
shell-bank further up Ferreira’s River, and near Cradocktown. At
this place the deposit rests upon a bank of drift, with bands of large
angular pieces of quartzite; this drift overlies a loose gritty sand-
stone. In the drift there are scarcely any indications of fossils ; but
in the deposit above there are strata of innumerable shells in a sandy
calcareous matrix. This shell-bed, capped with a red clay, several
feet thick, is the most prolific portion of the deposit we are now
treating of. The shells are all perfect, with the most delicate orna-
ments preserved.
With the exception of a Psammobia, none of the shells found here
have, up to the present time, been found on the shores of the bay.
Still, in the whole series of shells collected, there is a nearer ap-
proach to those of the present ocean, while there is a marked
difference in character between these fossils and those obtained from
the Akera-stratum.
These shell-deposits at Ferreira’s River &c., must have been laid
down in the waters of a bay, stretching from the Zwartkops to the
Port-Elizabeth hills, and extending some miles inland. On the in-
tervening ridges no signs of them are to be traced. In fact, it
seems almost certain that the ridges must have stood out of the
‘surrounding waters as islands. This is remarkably the case at the
creek, where the high ridges alluded to will be seen. When stand-
ing on the shell-bank at Ferreira’s River, one cannot help being
strongly impressed with this idea, and that the sea must have
been as calm there as in a land-locked bay, protected as it evidently
was from the roll of the open ocean. The appearance of the
shells themselves strengthens this view of the case, from the
beautifully perfect state in which almost all of them are found—
with all their most delicate outlines preserved, and the bivalves
almost invariably having both valves uninjured and closed. These
520 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
indications must surely prove that here they must have been de-
posited in still water, below or beyond the influence of the tidal
and other waves; while, on the other hand, the shells of the
“raised beach” appear to have been deposited on a kind of
outer reef, exposed to the full force and constant action of the
sea, which broke them into fragments, and rounded off their fractured
edges.
§ 4. The Red Clay.—The deposit which-seems to follow these
is the red clay, as shown at gg, in Section O (fig. 4). The exact
position of this clay, to which I have before alluded (p. 518),
requires more careful examination than has yet been given to it.
There appears to be little doubt, from the section just referred to,
that it must be more recent than the shell-deposits we have been
describing ; for upon the flat, at a little distance from the north end
of Port Elizabeth, they are found cropping up through it. These
shell-beds, judging from their fossils, are identical with those of
Ferreira’s River. However, as I have said, little is at present known
of this clay, except that it varies considerably in thickness in different
localities: thus it may form merely a superficial covering to the shell-
banks mentioned; while the late Dr. Rubidge informed me that at the
New Prison it is some 60 or 80 feet thick ; and, at Oliphants Hoek,
Dr. Atherstone states it to be 100 feet. Whatever may be its thick-
ness, it must have been deposited under totally different cireum-
stances from any thing preceding it. The transition from the one to
the other is so sudden that, with the limited information we have
about it, it will have to be left to future investigation before its
history can be written, as well as to discover (what is probably the
case) deposits on other parts of the coast that may intervene be-
tween the shell-banks and the clay, and others between the clay
and the formation which follows, thus more clearly explaining the
changes that led to its deposition.
§ 5. Latest Shell-beds.—The next known deposit of the ancient
sea is that marked C,C, in section T No.1, and Cin T No. 2. This
is evidently the most recent, previous to the existing order of things.
In the Bight, as shown in the section, it is found in detached mounds
of drift-sand, with a thick horizontal bed of shells on the top. These,
however, from their position and structure, are merely the isolated
remains of what, at one time, was a continuous and wide-spread de-
posit. It is found on different parts of the coast, and is especially
remarkable on the south side of Port Elizabeth, towards a small in-
dentation called the Shark’s-River Mouth. In this locality the quart-
zite rocks (near the top of the ridge, and at an elevation of 180 feet
above the sea) have been worn away to a long slope by the action of
the waves &c. About one-third up the ascent, and resting upon the
quartzite, is a mass of conglomerate composed almost entirely of
quartzite fragments imbedded in limestone, with fragments of shells.
There is another accumulation of conglomerate at the same place, at
a lower level, composed of waterworn pebbles. These conglome-
rates have been found at other parts of the coast. Upon this con-
glomerate, or, where it is wanting, upon the quartzite itself, are
STOW—-SOUTH-AFRICAN GEOLOGY. 521
high mounds of sand, such as those before alluded to, with immense
masses of shells imbedded in their upper portions.
Some of the shells, although identical with those now living on
different parts of the coast, are not now as numerous on this particular
part of the coast as they were when the shell-mounds now under
consideration were deposited; they are, however, still very numer-
ous in other, but somewhat distant, bays.
Some have supposed that these accumulations, at such elevations,
are somewhat similar to the “ kitchen-middens” of Denmark; and
they wish to account for this immense accumulation of shells by
imagining that they are the remains of the feastings of some an-
cient races who at some time inhabited the sea-coast. But, after a
careful study of the locality, I cannot arrive at the same conclusion.
These shells, judging from their appearance, must have been deposited
by the sea where they are now found. The quartzite has been (as
before mentioned) worn away until it forms a long steep slope of
some two or three hundred yards. The rush of the tidal waves over
the surface of this rock (and they have left evidence of their action)
would sweep every thing off it; and their recoil, carrying the shells
and sand to the lower levels, would deposit them there in compara-
tively quiet water, and thus form the stratum we now find.
Between this spot and Port Elizabeth, there are a number of
places where this same band of shells is exposed; but in these
instances there is a deposit of sand many feet thick above it. At
the spot to which I am now confining my remarks, however, this
upper deposit has been denuded, or blown away, leaving the large
masses of shells I have described exposed on the surface. Here
and there they look, at first sight, as if they had been placed in
piles; hence, no doubt, the mistaken opinion about them; but on
examining these detached heaps, they are found to be parts of the
original deposit, the surrounding and intermediate portions having
been worn away, and the shells having become broken and pulverized
by atmospheric influences. There can be little doubt that at one time
the exposed portions of this shell-deposit were covered, as before
suggested, with a thick layer of sand; for in many parts very large
quantities of fossilized roots, stems, and branches are spread over
the shells. Specimens of these must, from their perfect state of pre-
servation, have grown on the spot, and could not have been washed
from a distance. In some instances, where the sand is left, they
are still partially enveloped in it. The probable cause of the change
they have undergone has been that the water which permeated
through the sandy and shelly soil in which they grew, became so
charged with lime that, when the roots &c. decayed, the carbonate
of lime itself was deposited, as in a mould, in the spaces left; and
these casts, when the sandy matrix was removed, either by strong
winds, which so often prevail along the coast, or by other causes,
have been laid bare. I have found the same on the coast to the
east of the Great Fish River.
Numbers of teeth and bones are frequently discovered imbedded
in this shell-deposit near the Shark’s River. The position in which
§22 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
these are found would also tend to prove that they and the shells
were entombed together by aqueous agency, and that they were not
the refuse of the repasts of a primitive race. Thus the bones were
perfect, and, in some instances, large portions of the skeleton were
together in the proper positions, not scattered and broken, as they
would have been had some savage been feeding on them. Unfor-
tunately these relics would not bear removing, but broke up into
small fragments as soon as they were dug out and handled.
The facts here stated must, I think, satisfactorily prove that
these shells have been accumulated in the position they are now
found in by the cause and in the manner here assigned. This de-
posit is one of the latest, if not the very latest, prior to the last ele-
vation of this part of the South-African coast, and must have
immediately preceded the present order of things. Since that time
a gradual emergence of at least 150 feet must have taken place—
since the ocean-waves broke upon and wore away the sloping
quartzite rocks before mentioned.
Table of Postpliocene and Recent Deposits between Port Elizabeth
and the Zwartkops.
Feet. Name. Remarks.
20 to 30......... Shell-deposits with bones | Raised 60 or 70 feet above
and fossil wood. the present level of the
sea. AJl the shells are
the same as those now
found on the South-
African coast.
30 to 100 ...... Red clay.
About 25 ...... Shell-bank at Zwartkops | Panopea, Tapes, Solen,
Bridge. Mactra, &e.
Exposed 6...... Raised beach near the | All the shells broken.
Zwartkops mouth.
15 to 18......... Shell-bank at Ferreira’s | All the shells perfect. Zo-
River. ripes, Tapes, Cardiwm,
Cerithium, &e.
18 to 20......... Drift and gravel upon | Angular pieces of quart-
which one portion of zite, intermixed.
the last shell-bank rests.
1S carat ce see Strata at the Bight, Port | Akera, Cerithium, &e. &e.
Elizabeth.
STOW—SOUTH-AFRICAN GEOLOGY. 523
3. On some Pornts in Sourn-Arrican Grotoey.—Parts IT. and III.
On the Dicynopon or Karoo Formation—its Forest-zones, as
shown by Sections in the Winterberg and the Stormberg (Dor-
drecht, Upper Kei River, and Klaas Smit’s River), and its De-
nudation by Ice-action; with Remarks on the Climatal changes
Pap etl Africa. By G. W. Stow, Esq., of Queenstown, South
ica.
(Communicated, with Notes, by Prof. T. Rupert Jones, F.G.S.
My P
[Read December 7, 1870 *.]
Part I].—Tue Forest-zones AND OTHER STRATA OF THE Dicynopon
FoRMATION.
In the Dicynodon (Karoo) formation t we find two or more
distinct forest-zones in this eastern part of the colony. At Dordrecht
(Albert), in the Upper Stormberg range, on the south of the
Kaga Mountain (an offshoot of the Winterberg, in East Somerset),
in the Kroome range, and in the Amatola Mountains (British
Kaffraria) a thick and gritty sandstone frequently makes its
appearance on the slopes of minor valleys, and on the flats at the
same line of elevation; and wherever it is exposed there is almost
invariably an abundance of fossil wood. Near Greytown and the
Kabousie nearly entire trunks of trees have been discovered. Near
the Kom-Kom, a branch of the Kaga River, I have collected
numerous specimenst.
Section at Dordrecht.—In the section (fig. 8) the portions marked
a, a,a are covered with débris. No.1 protrudes in enormous masses
of greenstone or basalt (“‘ ironstone” of the colonists), which, judging
from the line of exposure, must be conformable with the strata
on which they seem to rest§. About 50 feet below, a rather com-
pact sandstone is exposed, resting upon a claystone (No. 2)|j, about
two feet thick; this, again, upon No.3, a coarse-grained greyish
sandstone 4], twelve or fourteen feet; and immediately beneath this
is No. 4, grey indurated shale. Below this is a coarse friable
brownish sandstone (No.5), resting on No. 6, which is very similar,
but full of ferrugimous patches and nodules, specimens of which
are sent**. Many of these nodules are filled with ochres, fine im-
* For the remainder of the papers read at this Meeting, see pp. 49-73.
+ For Mr. Stow’s description of a section of the Karoo beds of the Rhenos-
terberg, an offshoot of the Sneewbergen, see Quart. Journ. Geol. Soc. vol. xy.
p. 194.—T. R. J.
t Several segments of probably coniferous trunks were sent by the author.—
Rae: :
§ The specimen of No.1 sent is a small exfoliating nodule of greenstone.
—T. R. J.
|| The specimen of No. 2 sent isa piece of felspathic trap (claystone).—T. R. J.
{ With felspathic cement.—T. R. J.
¥#* “T), §. 2.” Nodules of quartz grit, with some felspar, cemented with iron-
oxide, showing transverse lines of stratificatiou externally, and containing ochre.
—T. RB. J.
PROCEEDINGS OF THE GEOLOGICAL SOCIETY,
524
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STOW—SOUTH-AFRICAN GEOLOGY. 525.
palpable powders of different colours, from which the ancient Bush-
man race (now rapidly becoming extinct) obtained many of the
pigments they used in their cave-paintings. This noduliferous
sandstone lies on the quartzose grit (D. 8. 1*, in some places
almost a conglomerate), No. 7, ten feet thick, and composed of
quartz, which could only have come from the Washbank. Below
this is the coarse sandstone of the “ Forest-zone,” No. 8, with “ silici-
fied” trees, probably coniferous, at least thirty feet long. No. 9is a
much finer-grained sandstone, and of a darker colour. Great num-
bers of what appear to be casts of rootsf, are obtained from this
deposit. Sometimes they are soft and easily pulverized; and when
found in that state they were ground down and used by the
Bushmen as a fine dark chocolate paint, frequently used by them in
delineating the human figure in their caves. The height from the
lowest exposed stratum to the basaltic blocks is about 450 feet.;
The discovery of stratified clays below these beds was made in
sinking a well in the village of Dordrecht ; and although no inter-
vening section has yet been obtained, it seems very probable that
they are conformable. For six or eight feet the upper clays are
of a bright-yellowish colour, No. 10, with abundance of Pecopteris (?)
and other plants. I secured a large case of them; but, unfortunately,
during its transit it was saturated with rain, and these beautiful
specimens were destroyedt. Below, the clays (from seven to eight
feet thick) are of a light-grey colour, No. 11; here the Ferns &c.
are not so abundant. Below this there is a dark bluish-grey clay,
No. 12, much more compact than those above, and from ten to twelve
feet thick ; in this the leaf-impressions are far less numerous. I
am not aware whether or not these clays appear at the surface at a
lower level.
The dip of the strata in the section just described is 6° or 7°S.E.,
and they are probably some of the most recent on the northern
portion of this great basin of deposit.
Section on the Upper Zwart Ket.—The section, fig. 9, is from the
* «7.8.1.2? Round lump of coarse quartzose grit (some of the grains
rounded), with some felspar and a little mica, feebly cemented with iron-oxide
and some clay.—T. R. J.
t The specimen sent represents, in fragments, a long subcylindrical con-
cretion (?) of amorphous chocolate-brown hematite, striated longitudinally
outside, and here and there showing traces of concentric structure within.
Specimens of the enclosing rock, sent with the above, consist of ferruginous
sandstone, with indeterminable casts and markings.—T. R. J.
{ Mr. Carruthers, F.R.S., of the British Museum, having examined the speci-
mens here referred to, has kindly supplied the following note :—
“The specimens from Dordrecht are not satisfactory. Among them are three
species of Ferns, which, I believe, are new. One seems to be a species of
Daneopsis, a second a Sphenopteris; and I know not what fossil genus I could
refer the third to. With these are associated what appear to be fragments of a
monocotyledonous plant, which are undeterminable.
“Tt is not improbable that a set of these Ferns would comprise specimens with
fructification ; and this would be very important. The fragments before me have
been so much injured by the water which had access to them that they are little
more than determinable as Ferns.
“The woods are all, I believe, Coniferous,—W. C., April 10, 1871.”
PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
526
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STOW—SOUTH-AFRICAN GEOLOGY.
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528 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
opposite side of the same basin—namely, from the Upper Zwart Kei,
north of the Winterberg, and 60 or 70 miles 8.S.W. of Dordrecht.
The sketch map (fig. 10) is to explain how the sides of this range of
hills are worn away, rising from the more level ground to the
top of the ridge. In the section the outlines of the Great Win-
terberg and the Groot Tafelberg are shown in the distance, to mark
the relative positions in which they are seen from this point.
On the top of this ridge is found at 14, 14, a mass of enor-
mous blocks of disintegrated basalt cappingitsedge. Similar blocks
are found at a lower portion of the ridge resting on No.9. No.
13 is a very hard compact sandstone, weathered into vertical
lines until it has assumed an almost columnar or basaltic appear-
ance; but on being broken, it displays distinct lines of horizontal
stratification. It forms a precipice some 30 feet high along the
face of the hills. Below this is a coarse-grained sandstone (No. 11,
11), sloping away to the bed of shale (No. 10) immediately under-
lying it. This shale is upwards of 200 feet thick, and of a much
darker colour than the shales below ; no fossils have yet been found
in it. It forms a sloping shoulder all along the hills, as shown on
the left of the section; and its position in the map is at 10,10,10. It
rests upon a coarse-grained sandstone (No. 9), the exact thickness of
which is unknown. This covers a sandy shale (15), about eight feet in
its thickest part, and gradually thinning out. In this shale (15) Mr.
Donald White discovered the fragment of bone D. 8.39*, and the fossil
D.8. 40*. Below this is a shale (7, 7, 7), varying in thickness, and
about 20 feet where thickest, interlaminated with thin streaks of
bluish clay, and near the top discoloured with innumerable specks of
carbonized matter. No. 6 is a gritty greyish sandstone (specimen
D.8. 45*), about 200 feet thick. This becomes exceedingly coarse-
grained in the uppermost beds. In its lower portion were found the
reptilian skull (D. 8. 35*) and the fragments of bone (D. S. 36 and
37*) ; at the spot marked “5” the lowest band is quite a plant-bed,
of which D. 8. 38 and D. 8. 43 and 44 are specimens*.
No. 4, beneath this, is a concretionary sandstone (see specimen
D. 8. 46*), containing fragments of shale and quartz, together with
nodules, such as those sent? (Nos. D. 8. 29 to D. 8. 34). Three
beds of similar rock occur in the outlier 6. At one spot, as in
stratum 3, it appears as if the shale had been cut through by some
stream or current down to the sandstone beneath, and the nodular
sandstone (4) deposited in the space thus denuded. If this supposi-
tion be correct, the banks of this ancient stream must have been at
* D. 8.35. Small skull in sandstone, with calcareous cement. 36. Bone in
similar sandstone. 37. Bone in concretionary calcareous sandstone. 38. Fine-
grained concretionary calcareous sandstone as above, with Calamites(?). 39.
Sandstone, with calcareous cement, containing bone. 40. Tooth in calcareous
sandstone, as 89; the other part of the specimen is greenstone. 43 and 44.
Fine-grained sandstone, with highly calcareous cement, and containing Peco-
pteris(?). 45. Fine-grained sandstone. 46. Concretionary, fine-grained, cal-
careous sandstone, with some films of shale.—T. R. J.
t Sandy, chatoyant, radiating calcite.—T. R. J.
STOW—SOUTH-AFRICAN GEOLOGY. 529
least 25 feet high. But whatever may have occasioned this deposit,
the other beds (4, 4, 4) have had a similar origin.
It was in the lowest bed of shale (3, 3, 3), especially at 3a, where
it is 25 feet thick, and of a reddish colour*, that the greatest quantity
of reptilian remains were found. Some of them appear to belong to
undescribed animals; others, from a cursory view, seem as if allied
to Micropholist. Nos. 26 and 27 are remarkably beautiful and
perfect, showing rows of exceedingly minute teeth. No. 24 seems
almost identical with another little skull that was obtained from
the rocks near Whittlesea, most probably a continuation of the same
strata. The portions of the reptilian skeleton (D.S. 10 to D. 8. 16)
are also exceedingly interesting, on account of the perfect preserva-
tion of the bones of one of the legs. When first got out of the rock,
a few of the bones of the foot were attached; but these were unfor-
tunately lost in removing them: even those that are left seem to
characterize an animal of more terrestrial habits than many of those
already known.
It is to the energetic zeal of Mr. Donald White that I am indebted
for the valuable specimens marked respectively D. 8. 10 to 40 and
43-47, and also for much valuable information with regard to this
locality t+. At the spot marked 3a he obtained nine skulls in the
course of one day’s search.
The denudation of the lower part of this range of hills is very diffe-
rent from that of the higher part occupied by the shale “10.” The
sandstones, interbedded with the shales, are cut into along the range
by numerous kloofs orravines—the strata forming projecting shoulders
between them (as shown in the map, fig. 10), and rising in steps from
the more level ground to the slopes of stratum 10, thus forming
a marked contrast to the latter.
Below the fossiliferous shale (3), and just below where it is the
thickest, the sandstone, a few feet in depth, has a purplish-grey tint
(No. 2, 2), asif a portion of the colouring-matter of the shale above
had permeated the sandstone to that depth; below and continuously
with this the sandstone is fine-grained and yellowish, and is the
lowest exposed rock of the series.
The outlier 6 is somewhat different in character from the range
of hills. Init the shales are wanting, except at the point 7; and
they are replaced in a great measure by the sandstone (4, 4, 4) before
described, and which we may imagine to be the deposit of a current
deflected from time to time from one part of the area to the other.
On the opposite side of 6, and also round the shoulder of the
mountain at D, the shales are much more largely developed than on
this side ; but no section has yet been made of them.
Further, three dykes (12) traverse the outlier, converging towards a
* Very fine-grained, purplish-red, nodular, argillaceous sandstone, calcareous
near the bones.—T. R. J.
Tt Quart. Journ. Geol. Soc. vol. xv. p. 642.
{ The specimen marked D.S. 41 (large skull, in two fragments of rock)
was given to me by Mr. Powell. The specimen D. 8. 42 was found by myself
at the Queenstone Quarries; it is of hard grey sandstone, with a large plume-
like plant on it.
» VOL, XXVII.—PART I. 20
530 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
central point at the top (see map, fig. 10). There is no displacement
or alteration in the composition of the strata where they come into
contact with the dykes. Dr. Rubidge thought that such dykes were
formed by cracks due to the shrinking of the strata, and filled up in
the same manner as deposits are supposed to take place in some
mineral veins.
The combined thickness of strata in the two sections (figs. 8 and
9) amounts to about 1200 feet for this portion of the Dicynodon
or Karoo formation; but this is evidently but a very small part of
their entire thickness ; for, taking the dip from the Zwart Kei to the
Stormberg, at angles varying from 4 to 7 degrees towards the N.W.,
and on the Dordrecht side of these mountains, dipping at the same
angles towards the 8.E., it is highly probable that the central
thickness of this portion must be enormous. Very little will be
known of their true history until the sections of every intervening
mountain-side are fully described. Some time, however, must elapse
before this can be accomplished, as many parts of the country are still
occupied by the native tribes.
Dr. Livingstone’s discoveries seem to throw some light on the
origin of this formation, viz. an elevated plateau, with successive
chains of lakes and marshes, that have been silted up, and subse-
quently the basins we find in the present day denuded out of the
strata thus formed.
Accompanying the fossils mentioned in this paper, I have sent a
packet given to me by Mr. C. W. J. Powell, and collected by him
near the Upper Zwart Kei*. The large skull, so remarkable for
its peculiar rows of small teeth (D.8. 41. Probably Labyrinthodont.
—T. R.J.), was also found in the same neighbourhood by Mr.
Powell; but I am not able to point out the exact strata from which
any of these were obtained. I have also enclosed casts of stems
from Kneehalter’s Neck, given tome by Mr. John M‘Donald +.
Section of the Stormberg on the Klaas-Smit’s River.—After finish-
ing my account of the Dordrecht and Zwart Kei sections, I obtained
much valuable information with regard to a section of part of the
south face of the Stormberg from Mr. Charles Evans ¢, who has ex-
plored a large portion of the range in search of coal.
This section (fig. 11) illustrates some of the strata between the
other two, near the synclinal axis of what I will term “the great
Stormberg basinӤ.
* No.1. Rippled, fine-grained sandstone. 2. Ferruginous sandstone, with
obscure surface-marks. 3. Very fine-grained sandstone, bearing mud-ripples.
4h ae with cast of Calamites or Equisetites? 5 and 6. Obscure casts.
t Nos. 7, 8, and 9. Sandstone casts of small portions of striated stems
(Equisetites or Calamites ?).—T. R. J.
{ For some notes by Mr. Evans of Queenstown, on the Coal of the Storm-
berg, see the ‘ Mining Journal,’ Jan. 14, 1871.—T. R. J.
§ It is worthy of remark that, as in other instances more numerous than they
were once thought to be, the Stormberg range is a synclinal mountain ; for, as has
been shcwn at Dordrecht, Buffel Doorns Flat, &c., the strata of the north and
south dip towards and into it.
STOW—SOUTH-AFRICAN GEOLOGY.
531
Fig. 11.—Section on the South Side of the Stormberg, at the source of
Klaas-Smit's River.
ates
a
Height almost 1075 ft.
a. Trap dyke.
6. Trap capping the Hangklip.
c. Strata not examined.
1. Rather deep brownish-red shale.
2. Sandstone.
3. Light brownish-red shale.
4. Sandstone.
5. Shale, lighter than Nos. 1 and 3.
6. Sandstone, with leaves and wood,
coal and black shale.
7. Light-brown hard shale.
8. Alternate layers of light shale and
coarse sandstone.
(Sia qur1049 943 Jo
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S
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. Sandstone.
. Black shale, with seams of coal.
. Pipe-clay.
. Bluish-brown clay.
. Gritty ferruginous sandstone.
. Ironstone nodules.
. Rather fine grey sandstone.
. Dun-coloured shale.
. Yellow clay.
. Very fine-grained sandstone.
. Light-coloured shale.
. Kine-grained sandstone.
202
532 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
This section is from that part of the mountains where the Klaas-
Smit’s River (the “Hokili” of Hall’s Map) takes its rise. The
better to explain its position relatively to the two others previously
described, I send a rough sketch-map of the intervening country,
fig. 12).
The Tee exposed stratum (1, 1) is a rather dark brownish-red
shale, about 150 feet thick, full of minute specks very much resem-
bling mica. On this is a very fine-grained greyish sandstone.
It forms a precipice about 40 feet high ; and this is the case with
every succeeding sandstone, the shales sloping from the one sandstone
to the foot of the other, which rises at once precipitously 40 or 50,
and, in the case of stratum No. 6, nearly 75 feet, forms a kind
of terrace a few feet wide, or, as on the surface of the last-mentioned
stratum (6), one of several yards in width, and then slopes up again
to the foot of the next sandstone at the higher level. No.3 is a
shale of about the same thickness as the one below, and very similar in
character, except that it is of a lighter colour. Upon this rests a
sandstone (4) containing abundant impressions of leaves and very
thin layers of fossil wood. The next shale (5) is still lighter in colour
than the preceding one. Over this is No. 6, a rather gritty, light-
brown sandstone, also containing numerous impressions of leaves,
similar to those found in No. 4, as well as fossil wood; also streaks
of fine coal and black hardened shale. These small patches of coal
appear to have been accumulations of vegetable matter in hollows
on the uneven surface of the sandstone beds at the time of deposi-
tion. Above this is a bed (7) about one foot thick, composed of thin
layers of a light-brown hard shale; a number of thin alternate layers
(No. 8) of light-coloured shale and coarse sandstone, containing round
nodules and pieces of fossil wood, succeed. These nodules contain
the same kind of ochres as some of those found in the Dordrecht
section (page 525), the contents of which were made use of by the
Bushmen. Next comes a thin sandstone (No. 9), and upon that six
feet of black shale (No. 10), containing a number of seams of coal
varying from an inch to a footin thickness. Thisis the “ Stormberg
coal deposit.”” I have seen a spot where this coal-shale is 14 or 15
feet thick. It is found cropping out at intervals for many miles
along the face of the mountains; it also reappears on the northern
side of the range; but the sections on that face have not yet been
examined. In this deposit (at 11) there is a remarkable band of
very fine yellow and white pipe-clay, about two or three inches
thick, its colour offering a marked contrast to the black shale and its
accompanying coal-seams. No. 12 is a stratum of bluish-brown clay,
almost shaly. No. 13 is a gritty ferruginous sandstone, contain-
ing nodules (very similar to those sent as specimens from Dordrecht)
and quartz-pebbles. Upon this lies No. 14, consisting of a thick
band of ironstone nodules. It has been thought that the infiltration
through these strata, especially No. 13, into the coal-shales below
has injured the quality of the coal found in them by impregnating
it with mineral matter, from which that found in No. 6, in the small
STOW—SOUTH-AFRICAN GEOLOGY. 533
Fig. 12.—Sketch-Map showing the relative position of the
Sections 8, 9, and 11.
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@. Position of Section at Dordrecht (fig. 8). 6. Position of Section on the Upper
Zwart Kei (fig. 9). ¢. Position of Section in the Stormberg (fig. 11).
534 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
hollows above described, is free. Above the bed of nodules rises an
abrupt precipice (about 40 feet high) of grey sandstone, of rather a fine
texture. Above this a dun-coloured shale (16), 140 or 150 feet thick,
slopes upwards to No. 17, which is a band of fine yellow clay about
a foot thick. From this another precipitous face of about 40 feet
(No. 18) of very fine-grained sandstone rises, and abovethis is a light-
coloured shale nearly 200 feet thick. No. 20 is another fine-grained
sandstone. The unexplored rocks above this rise some 500 feet, in
three successive tiers, as shown in the section. The precipitous
portions are sandstones; and it is highly probable that the intervening
spaces are occupied by shales. Near the foot of the mountain (at a)
a dyke makes its appearance, but, as in the other instances men-
tioned, without causing any change either in the position or
character of the rock through which it passes. The rocks here
described add another 1000 feet to those before mentioned.
The circumstance that makes this section of the Klaas-Smit’s
River of great interest is that here are found the first indications of
connecting links of the strata north and south of the Stormberg
range; and thus the equivalents of 4, 5, 6, and 7, near the bottom
of that part of the mountain now under examination, are to be found
almost at the top of the Hangklip (which is the culminating point of
some mountains nearly sixteen miles further south) immediately under
the precipice, at a height of 6500 feet above the level of the sea.
Further, the yellow clay at “17,” the gritty, noduliferous, and
ferruginous sandstone “13,” and bluish-brown clay “12,” remind
us of the very similar deposits found at Dordrecht (Section, fig. 8),
described at page 523 ; and it is to be hoped that before long other
sections may be obtained that will throw still further light upon this
interesting subject.
Part IJ].—Tue Crimatat coanexs or Soura Arrica (Hastern
PROVINCE AND THE VICINITY), AS INDICATED BY ITS GEOLOGY AND
Fossiis ; AND ESPECIALLY THE GiAcTAL DENUDATION oF THE KAROO
STRATA.
The consideration of the climatal changes that have taken place .
in this portion of the ancient world during the deposition of the
various formations treated of in the first part of this memoir will
lead me to make some remarks upon the probable cause of the denu-
dation of a large portion of the Dicynodon-rocks in the Hastern
Province.
Tertiary Climates—The evidence of the Pliocene shells of the
superficial limestone of the Zwartkops heights and elsewhere leads
us to believe that the climate of South Africa must have been of a
far more tropical character than at present. Take, for instance,
the characteristic Venericardia of that limestone: this has mi-
grated along the coast some 29 or 30 degrees, and is now found
within a few degrees of the equator, near Zanzibar, gradually driven,
as I presume it must have been, further and further north by a
STOW—SOUTH-AFRICAN GEOLOGY. - 535
gradual lowering of the temperature of the more southern parts of
this coast since the limestone was deposited.
During the formation of the shell-banks in the Zwartkops estuary,
younger than the Pliocene limestone, the immense number of cer-
tain species of shells, which have as yet been found living only in
latitudes nearer the equator, point to a somewhat similar though a
more modified change of temperature.
These, however, do not seem to have been the only periods when
this part of the world had a temperature different from that it now
possesses. In the Jurassic times the shells of the T’rigonta-beds in-
dicate a tropical or subtropical climate.
Nor are evidences wanting that there must have been vast
intervening periods when the climate approached to something
like antarctic severity. A question worth asking is, What can
have been the cause of the enormous accumulations of conglomerate
at Enon, at the sources of the Zwartkops, at Hankey, and elsewhere ?
Dr. Atherstone thus writes * of this formation at Wit-water river :—
“the whole range of hills was actually formed of these rounded
pebbles ;” ‘ the further we went the higher the cliffs became ;”
“‘ared clay formed the cement which bound them together ;” “ cliffs
200 or 300 feet high.” In the Kloofs at the sources of the Zwart-
kops this conglomerate is described by him as “ piled up 300 or 400
feet high;” at Venster-Hoek, Hankey, it is ‘‘ 740 feet high,”
“composed entirely of this Enon conglomerate,” with a matrix of
“soft red sand.”
Surely this enormous accumulation of water-worn pebbles} was
brought about by no common action of the sea-waves and ocean-
tides! but rather by the piling-up of worn fragments of rock on a
stormy ice-bound coast under an extreme condition of climate t.
Configuration and origin of the Karoo Beds.—During the last
few years I have had several opportunities of examining portions of
the Katberg and Stormberg ranges; and in many places they give
(as far as I can judge) strong evidences of having been subjected at
a remote period to the force of ice-action, and, indeed, that this has
been the great denuding agent of the Dicynodon-strata. After a
residence of nearly six years, the conviction has been forced upon
me that this denudation can be attributed to nothing else than to
the action of glaciers through an incalculable period of time. It
seems almost impossible that ordinary atmospheric agencies could
have eroded the surface so deeply and extensively, and carried away
vast tracts of strata that not only once occupied the area of the wide
plains and valleys now extending between the different branches of
* Eastern Province Magazine, vol. i. (1857), p. 523 &e.
+ The “Enon Conglomerate” has also been noticed by Bain and Atherstone
as occurring in the George district, Cape of Good Hope.—T. R. J.
{ The suggestion of Dr. Sutherland that the great breccia-band at the base of
the Karoo formation in the Cape Colony and Natal is a boulder-clay of glacial
origin (Quart. Journ. Geol. Soc. vol. xxvi. p. 514), is consonant with this view
of a severe antarctic climate having again and again obtained in South Africa.—
rend
536 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
the mountains, but may have even constituted unknown thicknesses
above their present tops.
With regard to the rocks themselves, of which these mountain-
ranges are composed, much is yet to be learnt, and to arrive at a
satisfactory conclusion about them will yet be the life-study of some
future geologist. Many questions of great interest and importance
have yet to be answered, thus :—Were these strata really of lacus-
trine origin? and if so, were these extensive and thick deposits
formed during a subsidence? If so, what were the outer barriers of
such wide-spread “lacustrine” deposits, effectually cutting off all
communication with the ocean during the deposition of sediments,
it is said, of some 6000 feet? Or were they laid down when the
region was considerably above the level of the sea? The Dicynodon
formation is cut across by the oblique sea-coast near the Gualana
River, and extends northward thence into Natal; its boundary
therefore on the south-east has disappeared in the present ocean.
Proceeding from the sea inland, through Albany, the country
rises In a succession of vast steps, as shown in the outline-section,
fig. 13.
The most recent of the Karoo deposits are to be found in the
Stormberg* ; and the whole face of this range (as is plainly seen on
approaching it) is composed of horizontal strata. Here, again,
the question arises, What could have formed the boundary of a
formation that shows so little evidence of displacement as the ele-
vated strata of these mountains? Again, Do these constitute one
continuous formation? Were they the vast deposits of a single
lake, or, rather, of many successive lakes? It is probable that, on a
closer examination, the latter will prove to be the case, and that
this extensive series of strata may be divisible into several limited
and overlapping groups of deposits. ‘To explain this, I have sent a
section (fig. 14) of that part of the formation to which this paper
principally refers. The synclinal structure indicates-that one basin
must have extended from the neighbourhood of the Katberg on the
south to near the Washbank on the north. Thus the dip of the
strata of the Queenstown hills is from 5° to 6°, and at the Bongolo Neck
5° N.N.W.; on an offshoot of the Stormberg, near the Buffel-Doorns
Flat, 5° N.N.E.; at the foot of the Stormberg 4° to 5° N.N.E.; while
at Dordrecht, on the other side of the mountains, at one spot the
dip is 4° to 5° §.E., at another 6° to 7° in the same direction, and
some twelve miles nearer the Washbank it is 5° to 6° S.S.E. These
dips seem to prove this particular basin to have its synclinal axis
somewhere about the centre of the Stormberg range, and that,
should the strata be continuous, the deposit must be of enormous
thickness.
Not only must the period of deposition of such rocks have been
of immense duration, but so also must that of their denudation,
from the time of the breaking of the original plateau (of which the
* Quart. Journ. Geol. Soc. vol. xxiii. pp. 143 and 172.—T. R. J.
t+ Such a plateau must have been similar to that in Dr. Livingstone’s ideal
section of South Central Africa.
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538 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
table-tops of such mountains* as the Winterberg, the Groot Tafel-
berg, the Twee Tafelbergen, Honder Neck, the Mostert Hoek moun-
tains, and Hangklip, near Queenstown, are the evident monuments)
to the excavation of the deepest valleys in the existing flats.
Whether or not all these Karoo strata were deposited under a uni-
form climate it is difficult to prove; but that there was some differ-
ence between the climate of the Dicynodon period and the present
seems to be indicated by the section (fig. 8) of the Upper Stormberg,
exposed near Dordrecht. These strata are now about 5000 feet
above the level of the sea. One bed, 10 feet thick, is composed of
a fine conglomerate of small fragments of quartz, and can be traced
wherever the side of the mountain is sufficiently bare. The only
locality, at present known, whence such quantities of quartz could
be derived is the Washbank. Immediately above and below this
band of conglomerate is a coarse gritty sandstone. The one above
is of a yellowish ochre colour, containing coarse nodules, such as
Nos. D. 8. 2 (D. 8. 1 is a specimen of the quartz-grit); in many
places it is discoloured with ferruginous patches. The one below is
the zone of fossil wood, which is found in abundance, evidently the
remains of a primeval forest. In some places there are trunks of
trees between 20 and 30 feet long, and great numbers of segments
erect in the position in which they grew; these latter are often
more than 8 or 9 feet in circumference. The fossil wood is found
wherever this coarse sandstone makes its appearance. The speci-
mens that have been examined are pronounced to belong to the
Coniferee. These last-mentioned strata are amongst some of the
latest of the Stormberg formation; and the wide-spread remains of
coniferous forests found there seem to point to climatal conditions diffe-
rent from the present, and still more different from those of the old
Carboniferous formations of Europe and elsewhere, the plentiful re-
mains of coniferous trees here most probably indicating that such
forests flourished in a more temperate climate. In such a climate
and in deposits formed under such circumstances it is not probable
that such abundant coal-measures would be found as those accumu-
lated in the northern hemisphere. From the wide extent of this
fossil wood it is evident that immense tracts of forest must have ex-
isted in those ancient times; but from that time to the present an
interval has intervened of incalculable duration, during portions of
which agencies (yet to be explained) have been in operation that
have not only occasioned the denudation above referred to, but have
also rendered the country a treeless region. ‘Trees introduced by
human agency thrive well; and it is not, therefore, the present cli-
mate that has caused the annihilation of forests: we must look to a
remote period for an explanation of this as well as the other pe-
culiar features of the country.
Denudation of the Karoo Beds.—The encroachment and retreat of
the sea cannot have effected the vast denudation, either during the
subsidence or the upheaval of the land; for there is no evidence that
any of the strata, except those on the immediate sea-coast, have
* These are all mountains of denudation and not of elevation.
STOW—SOUTH-AFRICAN GEOLOGY. 539
been subjected to oceanic agency: we must therefore look for other
causes to account for the vast alteration that the surface of the
country has undergone.
Some of the facts that I have been able to collect as bearing upon
the case are as follows :—
Katberg, and its Roches moutonnées and Moraines.—Commencing
with the Katberg range, we remark that the face of these mountains
on the south side, towards the sea, is generally abrupt and precipitous
(this is the case with most of the mountains of the Dicynodon forma-
tion), while on the north side, as seen along the road, the rocks are all
dome-shaped, or rounded and smoothed off, presenting a marked con-
trast to the opposite side. In the descent of the mountains on the
north side, on some of the shoulders and in a number of places at
high levels, are found large lateral accumulations of angular frag-
ments of rock, of various sizes, generally imbedded in clay. After
following the curvings of the long valley leading to Langfield, we
find large transverse mounds of drift and boulders, upwards of 60
or 70 feet high, that have afterwards been cut through where the
present watercourses run (see Section X). There are also large
deposits of unstratified clays, full of angular boulders of every size,
from small gravel and pieces of a few pounds’ weight to masses of
several tons, turned and tilted into every position. I have not had
an opportunity of carefully examining these fragments for strize
or groovings. In several instances I have found transverse mounds,
rising like small hills, in far wider valleys, and many miles from the
high mountain-ridges whence the boulders have apparently come. At
the Bolotwa, in the valley in which the Mission-station is situated, are
a number of detached “ kopjes,” formed of large boulders piled to-
gether, and imbedded, as far as can be seen, in a matrix of stiff,
black, somewhat loamy clay. Here also the boulders are mixed
together indiscriminately; in some parts they are very compact,
and numbers are of many tons’ weight. The largest of these mounds
has the side towards the top of the valley quite abrupt, and it there
rises to a height of some 70 or 80 feet. From the foot of this one
a bed of clay and boulders stretches for more than a thousand yards
through the Mission-station, where it appears to rest upon a loose
gritty sandstone (very similar to that at a place called the Bongolo
Neck, which I shall presently mention) in which large boulders are
imbedded. Again, some 12 miles nearer Queenstown there is a
high broken ridge of boulders, which the present watercourse of the
Inquobo (a torrent in rainy weather) cuts through at nearly a right
angle. A small section of this is exposed by a road-cutting; and
in two places the boulders are found resting upon stratified rocks
(shale), whilst in another they lie on a bed of the same “ whirled”
sandstone, with its imbedded boulders, as that at the Bongolo Neck
(see above) ; in some parts this ridge of boulders is from 900 to 1000
yards wide, and from about 90 to 100 feet high.
About a mile and a half from this, the whole surface of the preci-
pice along the range of mountains on the south side of the road is
smoothed and rounded off in a very remarkable manner. This is
540 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
just at a bend or shoulder, where a glacier, descending from the
northward, would press with the greatest force before turning off to
the watershed of the Komani or Inquobo just mentioned. But
there are many places where these rounded or dome-shaped rocks
are to be found. Thus among these same mountains, near where
the Zwart Kei passes through, they are found on both sides of a
gorge forming an outlet to an auxiliary branch of that river, near a
farm occupied by Mr. Lenard, and through which is an outlet toa
basin as large as, although more irregular in shape than, those of
Schaap Kraal and the Bongolo (see below). Of this outlet I have sent
a sketch (Y). Here the rocks are perfectly rounded off to the height
of several hundred feet; it is impossible to imagine how water alone
could have produced such an effect. Rocks with similar features
occur in another precipitous glen, forming the outlet of a large
valley-basin called Schaap-Kraal Hoek (vide infra), near Tarkastad.
In this case, on the one side all the rocks are smoothed and rounded,
while on the opposite side are beds of unstratified drift intermixed
with immense angular boulders. And here, again, we find a portion
of this boulder-clay resting upon the same kind of sandstone, with
its imbedded boulders and fragments of rock, as at the Bongolo
Neck.
Another notable instance of these dome-shaped rocks I noticed
on the road from the Rhenosterberg to Cradock. They were outliers,
forming small, rounded, bubble-like hills in the middle of a wide
flat valley some miles broad.
Basin-like valleys, their moraines, strie, gc. ; Schaap-Kraal Hoek.
—Another remarkable feature in the denudation consists of so-called
flats, but really basins, which seem to have been scooped out of the
horizontal strata. It is very difficult to understand how they could
have been so excavated by the simple agency of water, or the ordi-
nary atmospheric influences of any climate except an antarctic one.
Thus a place before mentioned, Schaap-Kraal Hoek, is an elevated
valley some 12 miles long and 6 or 8 broad; it is surrounded on
every side by a continuous range of mountains. The outer face of
all these mountains is exceedingly abrupt and precipitous, whereas
within the basin no precipitous rocks are to be seen; the sides are
all smoothed off, gradually sloping from the highest ridge towards
the centre, as if the strata that had once filled the intervening space
had been scoured out. The inner face of the highest. rocks, columnar
on the outer precipices, shows lines of stratification. (See section,
fig. 15.)
As the elevation of this valley is so near the level of the original
plateau, without any inlet through which water could have flowed,
one cannot imagine but that the denuding power must have been
some such agent as ice that accumulated within the basin itself.
Before the eroding of the outlet described above, a far more
ancient one existed where the road now passes towards Buissen’s
Spruit, a branch of the Eland’s River, and at the extremity opposite
to the present outlet. At both these outlets, where they debouch
into the lower country, the mountain-sides are loaded, to the height
STOW—SOUTH-AFRICAN GEOLOGY. 541
of several hundred feet, with large mounds of drift, containing an-
gular fragments of rock, intermixed with others more waterworn,
impressing one with the idea that they are, in all probability, the
remains of lateral moraines.
Fig. 15.—Section showing the denudation of the Schaap-Kraal Hoek.
(Section Z of Author.)
Watercourse.
1, 1. Abrupt escarpments of the outer face.
2, 2. Sloping surfaces of the interior.
3. Clay and other alluvium.
Bongolo.—The Bongolo valley, as well as a number of other large
valleys around Hangklip, are very similar in regard to the way in
which their interiors haye been denuded, and also in the precipitous
appearance of the outer side of their surrounding mountains. Hang-
klip, rising 6800 feet above the sea-level, seems to be the culmina-
ting height from which these radiate.
eee scratches.—The only place where I have distinctly noticed
grooyings on the surface of these rounded rocks was at a place
called Reit-Poort, in the Tarka; and here most of them were so
marked. The remote date of the denudation, and the nature of
most of the rocks, may explain why so few instances of ice-scratches
have yet been noticed.
Buffel-Doorns Flat.—The lines of drainage of the country do not
always appear to have been the same as at present, as during the
erosion of all these valleys there seems to have been a difference
from what obtains now, not only in the level of the interior of
these basins themselves, but also in their several outlets; this
is seen along the sides of the valley (Buffel-Doorns Flat) repre-
sented in section, fig. 16. Here we have three such openings,
at three different levels. On the outer side of these outlets there
are deep gorges cut through the mountains, leading generally to
other wide basins at a lower level; while these, again, are con-
nected, in the same way, with others of a less elevation than those
immediately above. The sides of these gorges are frequently covered
with heaps of huge boulders of every shape and position, drift, and
accumulations of unstratified clay. This succession of outlets is par-
ticularly well marked in this basin, on the southern slope of the
Stormberg, called Buffel-Doorns Flat. A number of other basins,
similar to this, situated among the branches of the same range,
have their present drainage through that of Buffel-Doorns. Almost
invariably all the inner faces of these basins are smoothed off, as has
542 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
-cast Sides of Buffel- Doorns Flat.
(Section A B of Author.);
dd. Projecting shoulders, appearing like raised terrace-beaches.
Fig. 16.—Seetion showing the successive outlets on the South and South
a, 6, c. Outlets.
been before mentioned with regard to
Schaap-Kraal Hoek, &c., with openings
generally tending towards the south or
south-east; the outer face of the moun-
tains surrounding them is precipitous and
abrupt, asis the case with those previously
noticed. If these, under a cold and ri-
gorous climate, were once filled with gla-
ciers, then one is led to believe that the
evidence adduced traces their course from
the upper valleys of the Stormberg, lower
and lower, from one level to another, until
they joined at Buffel-Doorns Flat. Here
this descending and united force appears
first to have broken over the lower barrier
at a (see section, fig. 16), or it may have
made its exit at all three openings, until,
either from greater pressure at the point
6 or some other cause, such as the more
rapid wearing of the rocks, the débris was
carried away to this lower level, until the
further erosion of c, reducing the level of
the drainage still lower, caused it to be
diverted finally in that direction. That the
level of the strata was at one time the same
as that of the respective outlets is clearly
proved by remains of them skirting different
portions of the plain, looking like the rem-
nants of so many raised beaches at the
different levels d d.
If the outlets of these different basins
were again filled up, the flats would form
a series of large lakes, each many miles in
extent. In fact they look, even now, more
like a number of drained lake-basins than
any thing else.
Another thing worthy of notice is, that
all the channels of the rivers of this por-
tion of the watershed of the Kei, such as
the Klaas Smit’s, the Zwart Kei, the Klip
Plaats*, the Imvani, &c., cut through the
different mountain-ranges at nearly right
angles. Along the sides of these openings,
* From the Klip Plaats Mr. Stow has sent
specimens,—No, 10, a coarse Dendrites, weathered
out on the face of a hard ferruginous sandstone
(like one sent by Dr. G. Grey: see Quart, Journ.
Geol. Soc. No. 106, p. 50), and No. 11, a piece of
fine-grained compact sandstone (quartz and fel-
spar), with the cast of a vegetable stem.—T. R. J.
STOW—SOUTH-AFRICAN GEOLOGY. 543
which are outlets such as I have described, extend for miles accu-
mulations of drift and boulders, very different from regular fluviatile
deposits ; and which seem to indicate that the erosion of the channels
in question arose from other causes than those at present in opera-
tion in South Africa*.
North of the Stormberg.—On the northern side of the Stormberg,
at Dordrecht and the Hot-Spruit (a branch of the Orange River),
the same features are equally observable,—the peculiar wearing of
the rocks; the large accumulations of unstratified clays, mixed with
patches of drift and boulders, both angular and waterworn; and the
rounding of the hills that face the interior of the valleys. I have
not yet visited the district of the Washbank; but Dr. Meintjes in-
forms me that among the mountains there, and which are the highest
portions of the Stormberg, there are distinct traces of both lateral
and terminal moraines. In a valley near Ladygrey, some 4 or 5
miles, wide, he found in the centre a patch of twelve or fourteen
enormous angular boulders, standing from 10 to 12 feet out of
the ground, and nearly the same in length and breadth. It would
have been impossible for water to have moved these masses of rock
to such a placey. The evidence in this part of the mountains
would refer to far more recent operations than those of which we
haye before spoken, as the last retreat of the glaciers would be along
this range, before the gradual change of climate caused their final
disappearance.
British Kaffraria.—Besides the evidence here brought forward,
there can be little doubt that an indefinite number of instances of
the same description might be collected among these mountains.
Not only here, but if we turn to the present coast we there find
numerous evidences of the same action that cannot be explained as
having occurred through the ordinary agency of water. Within a
few miles of Greytown, in British Kaffraria, there is a very remark-
able dome-shaped rock, situated on a neck or opening through a
high ridge, near the Kabousie. The rock runs across a portion of
this neck, and is completely rounded ; it is about 350 yards long,
and from 60 to 70 feet high. A number of huge boulders are
scattered about, as will be seen from the Sketch AC and Plan
AK, kindly furnished me by Mr. T. Liefieldt, Resident Govern-
ment-Agent of the Gaika Tribes. The high ridge on both sides of
the neck is perfectly smooth, and no other rocks are visible for
miles.
Kaga and Krome Mountains.—On the southern side of the Kaga
and Kroome mountains, branches of the Great Winterberg, we also
obtain evidence indicating that other agencies have been at work
besides those of a purely aqueous nature. Extensive flats are
* See the late R. N. Rubidge’s paper on pluvial denudation in South Africa.
Geol. Mag. No. 20, Feb. 1866, p. 88.—T. R. J
+ I have frequently seen large angular aati 10-12 feet in diameter,
with the uncovered part 9 or 10 feet out of the surrounding clay, in the centre
of a wide valley, where it would be impossible to explain how such ponderous
masses could have been transported by the force of water.
544. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
covered for many miles with clay, and innumerable angular frag-
ments of rock are thickly strewn over the surface. At Beaufort
this unstratified clay is from 30 to 40 feet thick. In Lower Albany,
again, similar angular pieces of rock are spread over a large extent
of country; some of the latter fragments I have found with one or
more polished surfaces. Some of the Dutch farmers offered to explain
the circumstance by stating that the polish was occasioned by the
wild bucks rubbing against them; but as they were often in such
positions that the bucks could not get at them, such an explanation
cannot be received.
Glacial agency.—Future investigations may modify some of the
conclusions I have arrived at; but here are a number of phenomena
that cannot be well explained by the theory of ordinary atmospheric
and aqueous agencies,—the rounding-off of the hills in the interior
of these ancient basins; the numerous dome-shaped rocks; the
enormous erratic boulders, in positions where water could not have
carried them; the frequency of unstratified clays; clays with im-
bedded angular boulders; drift and lofty mounds of boulders; large
tracts of country thickly spread over with unstratified clays and
superimposed fragments of rock; the Oliphant’s Hoek clay and
the vast piles of Enon Conglomerate—all these seem to indicate
periods when the climate was far more severe than at present:
these are phenomena, in fact, which in other countries are considered
to indicate accumulations and deposits requiring the wearing action
of ice and extreme cold to account for their production.
Succession of Periods dc.—Having thus tried to point out the
probable causes of the vast denudation of the Dicynodon strata, I
cannot help believing that it did not all take place at the same
period; the Enon Conglomerate and the enormous gaps that I
noticed as occurring between some of the different coast-formations
seem to point to this. Another evidence of the same kind appears
to be the remarkable ‘‘ whirled ” rock that I have alluded to (p. 539),
found on the north side of the Bongolo Neck. This rock was evi-
dently at one time the outlet of the present Quoquodala basin, before
the deeper opening towards Glen Grey was formed. In this place
we not only find unstratified clay with boulders, but this again is
placed upon what I have called a “whirled” sandstone, because it
looks as if, while it were yet soft, it had been stirred up, and rolled
together by ice enveloping the boulders imbedded in it (Section AD).
These last are mostly angular, and occur in every position, not
having been deposited according to size, as would have been the
case had water been the agent. This sandstone is evidently far
more ancient than the superincumbent clay, which appears almost
recent in comparison.
There seems little doubt that the whole of the Dicynodon forma-
tion, since the close of the period when its last strata were deposited,
has been high above the level of the sea, and its elevated position
has prevented any great accumulation of soil taking place; for since
the great denudation, and since the present transverse river courses
have been cut through the mountains (although, as I have before
STOW—SOUTH-AFRICAN GEOLOGY. 545
noticed, the closing up of these openings would turn large por-
tions of the present flats into wide lakes), there are no traces of
more recent lacustrine deposits that I know of; so that, with the
exception of the unstratified clays and boulder-clays, and a little allu-
vial soil, nothing is found, in this portion of the area, of later date than
the present drainage-system. This has, no doubt, tended in a great
measure to prevent a spontaneous renewal of timber-growth after the
extinction of the ancient forests (see p. 538), the soil having never
been renovated by new deposits formed beneath the ocean, as it has in
other countries. It must also be more difficult for the seeds of trees
and plants to ascend to an elevated plateau than to spread over
plains on a lower level, or just emerging from the waters.
Conclusion.—The foregoing collection of facts must, I think, tend
to prove that vast climatal changes have taken place during the de-
position of the various formations that have been brought under
review in this and the foregoing portions of my paper. It may be
objected that, with regard to such an extreme climate as is here
inferred, South Africa is too far removed from the present Antarctic
regions, and that the causes of great changes of climate are not un-
derstood.
The simple oscillation of the poles, however, taken together with
the continual and necessary alteration in the distribution of land
and water, would be surely sufficient to account for all the pheno-
mena yet known, changing not only the geographical configuration .
of the surface of the earth itself, but carrying with it the most im-
portant changes of climate over every portion of the earth.
In such a case, when the London area possessed a tropical climate,
the spot now occupied by Algoa Bay would be at some 68° south
latitude; or when the site of modern London was within or near
the Arctic circle, Algoa Bay would be within 5° or 6° of the equator,
with a temperature congenial to the existence of the large Veneri-
cardia of the Zwartkops Pliocene limestone (p, 534), In the former
case, South Africa would then possess (instead of mountains covered,
as at present, with snow for a few days in winter) an Antarctic cold,
with an ice-bound coast, and glaciers covering every portion of the
country.
Lastly, I have to notice in connexion with the geology of South
Africa the rare occurrence of the remains of either fish or mammals.
What has opposed their preservation? And further, was South
Africa the home of large Pachydermata during a period equivalent
to the Mammoth age?
Until within a very few years, the rivers of South Africa swarmed
with Hippopotami; and large herds of Elephants roamed over the
wide plains, which were also the home of the Giraffe and the Rhino-
ceros, and where the large Carnivora, Leopard, Panther, and Lion,
preyed upon the weaker animals. Are we, then, to find, in our
Pliocene deposits, Ostriches of gigantic size, enormous Lions, and
Elephants eclipsing the Mammoth itself—analogues of the great
Marsupials of Australia, the Mylodon, Megatherium, and Glyptodon
of South America, the Mastodon and Mammoth of the Northern
VOL. XXVII.—PART I. 2P
546 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
Hemisphere outvying the present inhabitants of those parts of the
earth? This interesting problem will have to be solved by future
geologists.
APPENDIX: ON THE PROBABLE EXISTENCE OF AN ANCIENT
SourHEeRN ContrrInEN’.
The many similar forms of life, either fossil or recent, that are
found scattered over various parts of different countries now so
widely separated by the Indian and Pacific Oceans, seem to indicate
that in very remote periods they must have been more intimately
connected with each other than they are at present.
To those who believe that all the species of the same genus, and
that in all probability all genera of the same family, have a common
origin, it will appear almost self-evident that it must have been so.
Thus remains of Dicynodont Reptiles and Labyrinthodont Amphibia
are found both in India and South Africa, “ affording,” as Professor
Huxley stated in a paper upon those from the former country, “‘ new
and interesting links with the fossil fauna of the Karoo beds of
South Africa.” In another paper he said, “There are two other forms
of Labyrinthodonts which exhibit many similaritiesto the Micropholis.
These are the Brachyops laticeps of Prof. Owen, from Central India, and
anew form allied to the Brachyops, but distinct from it, from Australia,
the Bothriceps australis.”
It is not only in the fauna of the Dicynodon formation, but in the -
flora also that connecting links are found; thus a Glossopteris that
has frequently been found in the Karoo and others from India
and Australia are so nearly allied to each other that a high
authority has stated that he “can find no specific distinction.”
With regard to this flora Mr. Tate, in his paper “‘ On’some Secondary
Fossils from South Africa,” says that it “presents. close analogy
with that of the coal formation of Eastern Australia, and the plant-
bearing beds of Burdwan and Nagpur in India. The charac-
teristic plant in each of these deposits is a Glossopteris; and it seems
that the Indian, Australian, and South-African plants are specifically
identical.”
Amongst the fossil Mollusca of the succeeding Uitenhage forma-
tion we find many other such connecting genera. Thus the Hxo-
gyra, Trigoma, Cucullea, Pinna, and Crassatella of the Sundays and
Zwartkops strata find their representatives in Mauritius, India, and
Australia, the Crassatella extending as far as New Zealand. With
regard to the plant-bearing beds of this series, Mr. Tate writes*,
—‘ ‘Of the four species of Pecopteris, one is not satisfactorily distinct
from P. lobata of India; and two others are closely allied to P. in-
dica, also from the Jurassic plant-beds of the Rajmahal Hills.
ec Asplenites lobata is common to these Indian and African
strata; and though, with one exception, they are distinct, yet, on
the whole, the Jurassic plants of South Africa recall those of Scar-
borough and the Rajmahal Hills.”
* Quart. Journ. Geol. Soe. vol. xxiii. p. 148.
STOW—SOUTH-AFRICAN GEOLOGY.
The Pectunculus and
Perna of the Zwartkops
Pliocene limestone, the
Cardium, the large Natica,
Loripes, Panopea, and
Akera of the more re-
cent formations, are found
spread over the same ex-
tensive areas as those pre-
viously mentioned. Of the
recent flora the ‘Ency-
clopedia Britannica’ gives
the following:—‘ On the
coast of Guinea and Congo
the flora is intermediate
between that of America
and Asia. Species of Sor-
ghum, Sterculia acuminata,
the Kela-nut, and the
Poison-bean of Calabar be-
long to this region.” “In
Chili there aremany genera
of Composites which are
also represented in Aus-
tralia and the Cape of Good
Hope.”
The most recent evi-
dences of an _ ancient
southern continent con-
sist most probably in the
wide-spread coral-reefs and
islands in the Indian and
Pacific Oceans, extending
from the southern portions
of the Red Sea and the
northern part of the Mo-
zambique Channel on the
west, to the Island of Ducie
in the extreme east, thus
including the Seychelles,
Madagascar, Mauritius,
parts of the coast of Aus-
tralia, New Caledonia, the
Pacific Islands, to the be-
fore-mentioned Island of
Ducie ; and on the north of
the Equator the Caroline
Islands, the Marianne and
Philippine Islands, the
Chinese Seas, along the
Fig. 17.—Outline Sketch taken from Andrie’s Neck.
Groot Tafelberg.
Twee Tafelbergen.
=
The dotted line ab indicates the level of the ancient plateau.
048 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.
southern coast of Sumatra, and the Maldives and Laccadives, on the
west of the Indian peninsula. As most of the species of the different
corals forming these reefs eannot exist in water beyond a certain
depth, the deep sea at present intervening between such widely
separated groups of islands would have formed an impassable barrier
to them; and thus the conviction seems forced upon us that most of
these coral-reefs are now crowning the tops of the ancient mountains
of a subsiding continent, along the shores of which the various genera
of shells and other animals could have migrated—as much as we are
impressed with the belief that the table tops of the Great Winterberg,
the Groot Tafelberg, the Twee Tafelbergen, and others previouslymen-
tioned (see sketch, fig. 17) prove the existence of the elevated plateau
that must at one time have occupied a large portion of Southern Africa.
Table of Elevations from Eland’s Post (Kat River) to the Banks of
the Orange River, near Aliwal. Taken by Mr. A. N. Ella, Go-
vernment Inspector of Roads, and Mr. J. Graham, of Aliwal.
Locality. Graham. Ella
feet. feet
Hland’s Post, Kat River ............ 2200
Katberg, highest point ofroad ... | —...... 5332
Ditto, flat on the north side, near i 4800
OAC canoe sancnnen wclcuspictenotene
Wilititleseayaefiseen vc ieeckn aca ce 3100
Qweens bo wan seed oc Mee ans eth or enveee tl enUme ee 3432
Klopper’s Fontein..................... 4600
Flat between Klopper’s Fontein and 4800
foot of Pen Hoek ...............
Foot of Pen Hoek, Stormberg...... | — ...... 5068
Seramenvi, GECKAG, GWG) soscoscca || We cocden 5596
Burshersdoxrpiy. nso: sieesssseseecuet il © eae eee e 4382
Alliiwall (ates AIS. a aR aes 4300
Banksof Orange River, nearAliwal | —_...... 4224
The flat around Bloemfontein, |
capital of the Orange River, 5300
JMRED SHEL cocoooscsanconcoaosccade [
Locality. Hall. Hall.
feet. feet.
The Great Winterberg is the cul- Gaika’s Kop,
minating point of the Kat and 7800 6800
Winterberg Mountains.........
Hangklip is the culminating point |
of the Andriesberg, an outlier 6800
of the Stormberg .....;......:.. J
Lieut. Sherwell.
Spitzkop or Compassberg is the |
culminating point of theStorm- | 10,259*.
berg and Sneewbergen .........
* Monts-des-Sources, in Basouta-land, is said to be the highest point in South
Africa ; but its exact height is not known.
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LIBRARY OF THE GEOLOGICAL SOCIETY.
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I. TRANSACTIONS AND JOURNALS.
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American Journal of Conchology. Vol. vi. Parts 1-3. 1870-71.
T. A. Conrad.—Notes on Recent and Fossil Shells, with Description
of New Species, 71.
T, A. Conrad.—Description of new Fossil Shells of the Upper
Amazon, 192.
Description of new Tertiary Shells, with Notes on Two
Genera of Lamellibranchiata, 199.
J. H. Redfield.—Catalogue of the known Species, Recent and Fossil,
of the Family Marginellide, 215.
American Journal of Science and Arts. Third Series. Vol. 1.
Nos. 3 & 4. March and April 1871.
C. King.—On the Discovery of actual Glaciers on the Mountains of
the Pacific Slope, 157.
S. P. Sharples.—On some Rocks and other dredgings from the Gulf-
stream, 168.
Baron von Richthofen.—On the Porcelain rock of China, 179.
T. S. Hunt.—Notes on Granitic Rocks. Part 2., 182.
O. C. Marsh.—On the Geology of the Eastern Uintah Mountains,
191.
C. M. Wheatley.—Notice of the discovery of a Cave in Eastern
Pennsylvania containing Post-Pliocene Fossils, 235.
KE. W. Hilgard—On the Geology of the Delta, and the Mud-lumps
of the Passes, of the Mississippi, 238.
W. M. Gabb.—Notes on the Geology of Santa Domingo, 252,
J. W. Dawson.—On Spore-cases in Coal, 256.
DG Mab snene: of a Fossil Forest in the Tertiary of California,
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C. F. Hartt.—Amazonian Drift, 294,
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Bath. Proceedings of the Bath Natural-History and Antiquarian
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H. H. Winwood.—Notes on the Rheetic Section, Newbridge Hill,
204.
Berlin. Monatsbericht der kéniglich preussischen Akademie der
Wissenschaften zu Berlin. February to April 1871.
Beyrich.—Ueber die Basis der Crinoidea brachiata, 33.
Ewald.—Ueber Ergebnisse aus der paliontologischen Untersuchung
einiger norddeutscher Neokomvorkommnisse, 78. ,
——. Verzeichnis der Abhandlungen der koniglich preussischen
Akademie der Wissenschaften von 1710-1870.
——. “Zeitschrift der deutschen geologischen Gesellschaft. Band
xxil. Heft 4. 1870.
A. Kunth.—Ueber wenig bekannte Crustaceen von Solenhofen, 771
(2 plates). ;
J. Lemberg.—Chemisch-geologische Untersuchung einiger Kalklager
auf der finnischen Schareninsel Kimito, 803 (1 plate).
KE. Kayer.—Studien aus dem Gebiete des rheinischen Devon, 841.
E. Weiss.—Studien tiber Odontopteriden, 853 (3 plates).
C. Rammelsberg.—Ueber den Meteorstein von Chantonnay, 889.
—. Ueber das Schwefeleisen des Meteoreisens, 893,
——. Ueber die Zusammensetzung des Lievrites, 897.
Ueber den Anorthitfels von der Baste, 899.
G. Berendt.—Das Auftreten von Kreide und von Tertiar bei Grodno
am Niemen, 903 (3 plates).
Band xxiii. Heft 1. 1871,
F, Zirkel.—Geologische Skizzen von der Westkiiste Schottlands, 1
(4 plates).
C. Fritsch.—Geologische Beschreibung des Ringgebirges von San-
. , torin, 126, .
C. Struckmann.—Die Pteroceras-Schichten der Kimmeridge-Bildung
bei Ahlem unweit Hannover, 214,
R. Richter.—Aus dem Thiiringischen Schiefergebirge, 281 (1 plate).
HE. Kayser.—Notiz iiber Rhynchonella pugnus mit Farbenspuren aus
dem Hifler Kalk, 257,
Breslau. Abhandlungen der schlesischen Gesellschaft fiir vaterliin-
dische Cultur. Abtheilung fir Naturwissenschaften und Medicin.
1869-70. ;
——. ——. Philosophisch-historische Abtheilung. 1870.
Siebenundyierzigster Jahres-Bericht der schlesischen Gesell-
schaft fiir yaterliindische Cultur. 1869. Breslau, 1870. .
F, von Romer.—Ueber die im Auftrage des kiniglichen Handelsmi-
nisteriums von ihm bearbeitete geognostische Karte yon Ober-
schlesfén, 34,
DONATIONS. 551
Breslau. Siebenundvierzigster Jahres-Bericht der schlesischen Ge-
sellschaft fiir vaterlindische Cultur (continued).
Runge.—Ueber die Salzfunde in dem norddeutschen Flachlande und
die geognostische Beschaffenheit des letzteren im Allgemeinen, 36.
- Ueber die Fortsetzung des oberen Jura im Regierungs-Bezirk
Bromberg, 38.
Ueber die neue Schrift des Prof. Zaddach: Beobachtungen
tiber das Vorkommen des Bernsteins und die Ausdehnung des
Tertiirgebirges in Westpreussen und Pommern, 39.
Websky.—Ueber Deformitaten an Quarz-Krystallen, 41. _
Bleisch.—Ueber ein neues Diatomeenlager in Schlesien, 76.
F. Cohn.—Nachtrag zu der Abhandlung des Herrn Dr. Bleisch iiber
das Diatomeenlager zu Pentsch bei Streuhlen, 160.
British Coal and Iron Trades’ Advertiser and Directory. Vol. i.
Nos. 7 & 11.
Builder, The. Vol. xxix. No. 1468.
Calcutta. Asiatic Society of Bengal. Journal. New Series. Vol.
sxx, No: 166.
——. ——._ Proceedings, No. 11. December 1870.
—. ——. —-. Nos.1&2. January and February 1871.
Canadian Journal of Science, Literature, and History. New Series.
Vol. xii. No.1. May 1871.
Canadian Naturalist and Quarterly Journal of Science. New Series.
Vol. vy. No. 3. September 1870.
G. Broome.—Canadian Phosphates considered with reference to their
use in Agriculture, 241.
T. Macfarlane.—On the Origin and Classification of Original or Crys-
talline Rocks, 304. ;
Geological Discoveries in Brazil, 342.
Chemical News. Vol. xxiii. Nos.591-603. March to June 1871.
Chemical Society. Journal. Second Series. Vol. ix. March to
May 1871.
Colliery Guardian. Vol. xxi. Nos. 534-546, March to June 1871.
Copenhagen. Det Kongelige danske Videnskabernes Selskabs Skrif-
ter, FemteRekke. Naturvidenskabeling og Mathematisk Afdeling.
Band ix. Parts 2-4. 1870.
Oversigt over det Kongelige danske Videnskabernes Selskabs
Forhandlinger, 1870. No. 2. .
Darmstadt. Notizblatt des Vereins fiir Erdkunde und verwandte
Wissenschaften zu Darmstadt, und des mittelrheinischen geolo=
gischen Vereins, Herausgegeben von L. Ewald. 3te Folge.
_ Heft 9. any
R. Ludwig.—Geologische Notizen zur Section Alzey, 127. °~
aurea eimie
552 DONATIONS.
Dresden. Sitzungs-Berichte der naturwissenschaftlichen Gesellschaft
Isis in Dresden. July to December 1870.
C. Bley.—Ueber den Rogenstein von Bernburg, 132.
H. Engelhardt.—Ueber einige Tertiirpetrefacten, 133.
——. Ueber den Liss in Sachsen, 136.
Geinitzi—Ueber das Vorkommen von Resten von Rhinoceros ticho-
rhinus und Elephas primigenius bei Dresden, 132.
——. Ueber Losskindlein aus der Lehmgrube zwischen Strehlen
und Mockritz, 182.
—. Ueber seine Arbeiten ftir die Herausgabe einer Monographie
uber das Quadergebirge in Sachsen, 134.
——. Ueber einige Petrefacten aus dem untern Planer von Plauen,
134,
——. Ueber Gletschererscheinungen in der Gegend yon Hoburg bei
Wurzen, 135. ;
——. Ueber Versteinerungen aus einer sandigen Ablagerung der
Kreideformation von Chateau de Meauene bei Lude unweit Angers
im Departement Maine-et-Loire, 149.
G. Klemm.—Ueber Concretionen und die bei Mineralien und Gestei-
nen auftretende Kugelform im Allgemeinen, 141.
Paine Palmacites Boxberge, Gein., truncus cylindricus, 150
1 plate).
O. Schneider.—Ueber einige Mineralvorkommnisse, 148.
Klemm.—Ueber die Braunkohlenablagerung von Beiersdorf bei
Grimma, 178.
Geinitz.—Ueber ein neues Vorkommen yon Steinkohlenablagerung
im obern Erzgebirge, 179. ;
Kinne.—Ueber die neuen geologischen Kartenwerke yon Ober- und
Nieder-Schlesien, 179.
Ueber Lorange in Norwegen, 182.
ee oet den Bergbau und dessen Werkzeuge in alter Zeit,
Florence. Bollettino del Reale Comitato Geologico d'Italia. Nos.
1-4. January to April 1871.
F, Giordano.—Sulla temperatura della roccia nella Galleria delle
Alpi Cozie (detta volgarmente del Cenisio), 1.
naa Cenni sulla costituzione geologica della Campagna romana,
G. vom Rath.—I dintorni del lago di Bolsena, 28.
T, TaramelliimSulla formazione eocenica del Friuli, 37.
G. Seguenza.—Intorno le formazioni primarie e secondarie della pro-=
vincia di Messina, 49,
T. Taramelli.—Osservazioni stratigrafiche sulle valli del But e del
Chiars6 in Carnia, 63. ays
I. Guareschi.—Intorno ad una resina fossile di Val d’Arno superiore,
B. Gastaldi—Scoperta del Berillo nelle roccie cristalline di Val
d’Ossola, 79. tani
Frankfort-on-the-Main. Abhandlungen herausgegeben von der
Senckenbergischen naturforschenden Gesellschaft. Band vii.
I’. Hessenberg.—Mineralogische Notizen, 1, 257 (9 plates): |
F, Scharft.—Ueber die Bauweise des Feldspaths. - Il. Der schiefspal-
tende Feldspath, Albit und Periclin, 47 (2 plates).
DONATIONS, 553
Frankfort-on-the-Main. Bericht tiber die Senckenbergische natur-
forschende Gesellschaft. 1869-70.
Geneva. Mémoires de la Société de Physique et d’Histoire Natu-
relle de Genéve. Tome xx. Part 2. 1870.
Geological Magazine. Vol. viii. Nos. 4-6, April to June 1871.
H. B. Woodward.—Inversion of Carboniferous Strata, Somersetshire,
149,
G. H. Kinahan.—olian Drift or Blown Sand, Ireland, 155.
C. E. de Rance.—Preelacial Geography of Northern Cheshire, 158.
H. Woodward.—Notes on a Visit to the Brussels Museum, 193 (1
plate).
W. Whitaker.—On the Chalk Cliffs from Seaford to Eastbourne, 198.
W. Davies.—Catalogue of the Type Specimens of Fossil Fishes in
the British Museum, 208.
J. Rofe.—Notes on the Crinoidea, 241 (plate).
8. Allport.—On the Structure of a Phonolite from the “ Wolf Rock,”
241; with a Chemical Analysis by J. A. Phillips, Esq., 249.
D. Mackintosh.—Drift of the Borders of the Lake-district, 250.
A. and R, Bell—The English Crags and their Invertebrate Fauna,
256.
G. H. Kinahan.—Metamorphic Rocks of Scotland and Galway, 263
(plate).
D. F orbes.—‘ On the Nature of the Earth’s Interior,’ noticed, 162.
ae Hennessy.—‘ On the Internal Fluidity of the- Earth,’ noticed,
216.
W. Carruthers.‘ Additions to Fossil Botany in Britain,’ noticed,
218.
“On the Discovery of Glaciers in Northern California,’ noticed, 269.
‘ Aoricultural Geology, Royal Agricultural Society,’ noticed, 271.
Dr. yen ‘Sun-Pictures of Rocky Mountain Scenery,’ reviewed,
173.
Palezeontographical Society’s vol. xxiv., reviewed, 175.
‘American Geological Surveys,’ reviewed, 178.
T. R. Jones’s ‘Geology,’ reviewed, 180.
Blyth’s ‘ Metallography,’ reviewed, 220.
‘ American Geological Surveys, Iowa,’ reviewed, 221.
‘Geological Survey of India,’ reviewed, 272.
‘Geological Survey of Michigan,’ reviewed, 275.
‘Geological Survey of Ohio,’ reviewed, 277.
Reports and Proceedings of Societies, 180, 225,
Correspondence, 189, 238, 285,
Obituaries, 240, 288.
Netes and Queries, 192.
Heidelberg. Verhandlungen des naturhistorisch-medizinischen Ver-
eins zu Heidelberg. Band vy. Heft 4. 1870.
Iron and Coal Trades Review. YVol.v. Nos. 160-165. March and
April 1871.
Linnean Society of London. Journal. Zoology. Vol.xi, No, 51,
1871.
—. -——. Botany. Vol. xi, No, 56. 1871
554 DONATIONS,
London, Edinburgh, and Dublin Philosophical Magazine. Fourth
Series. Vol. xli. Nos. 273-276. April to June 1871. From
Dr. W. Francis, F.GS.
Prof. How.—Contributions to the Mineralogy of Nova Scotia, 270.
A, Heim.—On Glaciers, 485 (plate).
London Institution. Journal. Vol. i. Nos. 4-6. April to June
1871.
Longman’s Notes on Books. Vol. iv. No. 65.
Milan. Atti della Societa Italiana di Scienze Naturali. Vol. xiii.
Fase. 1-3. 1870.
C. Marioni—Intorno ad alcuni resti di Ursus speleus della grotta di
Adelsberg, 55, 57.
G. Bellucci.—Avanzi dell’ epoca preistorica dell’ uomo nel territorio
di Terni, 149, ©
T. Taramelli.—Sugli antichi ghiacciaje della Drava, della Sava e dell’
Isonzo, 224.
a, Vol: xiv. Fase: I:- 1871;
Monthly Microscopical Journal. Vol. v. Nos. 28&29. April and
May 1871.
A. M. Edwards.—Microscopical Examination of two Minerals, 226.
Moscow. Bulletin de la Société Impériale des Naturalistes de Mos-
cou. Tome xlui. No.2, 1870.
Nature (Journal), Vol.iii. Nos. 73-78. April 1871.
W. M. Williams.—Papers on Iron and Steel, 374, 388, 410.
W. B. Carpenter.—Eozoon canadense, 386,
Fossil Cetacea, 392.
——. Vol.iy. Nos. 79-85. May and June 1871.
C. C. Bilake.—The Caye-Lion in the Peat of Holderness, 27.
J. B. Perry.—Hozoon canadense, 28.
Ven. Archdeacon Pratt,—Thickness of the Earth’s Crust, 28,
A. H. Green.—Thickness of the Earth’s Crust, 45.
D. Forbes.—Thickness of the Harth’s Crust, 65,
Paleeozoic Crinoids, 72.
W. King.—Kozoén canadense, 85.
H. Woodward.—Seeley on the Ornithosauria, 100.
Neues Jahrbuch fiir Mineralogie, Geologie und Paliontologie. 1870.
Hefte 6-8.
Hi. J. Burkart.— Ueber die Fundorte mexicanischer Meteoriten, 673.
A. v. Lasaulx.—Petrographische Studien an den vulcanischen Ge-
stemen der Auvergne, 693,
C. W. C. Fuchs.—Die alten Sediment-Formationen und ihre Meta~
morphose in den franzésischen Pyrenien, 719 (plate).
C. W. Giimbel.— Vorlaufige Mittheilungen tiber Tiefseeschlamm, 753,
F. Zirkel.—Mikromineralogische Mittheilungen, 802 (plate).
Zelger.—Ueher. Stylolithen, 833,
DONATIONS. 555°
Neues Jahrbuch fiir Mineralogie, Geologie und Paliontologie. 1870.
Hefte 6-8 (continued).
C. W. C. Fuchs.—Die alten Sediment-Formationen und ihre Meta-
morphose in den franzésischen Pyrenaen, 851 (plate). ‘
C. Schliiter.—Bericht tiber eine geognostisch-palaontologische Reise
im siidlichen Schweden, 929. ;
H, Credner.—Ueber nordamerikanische Schieferporphyroide, 970.
——. 1871. Heft 1.
R. D. M. Verbeek.—Die Nummuliten des Borneo-Kalksteines, 1
(3 plates).
R. Lincke.—Der Buntsandstein am Ostrande des Thiiringer Beckens,
15.
A. Stelzner.—Quarz und Trapezoéderfliichen. Hine paragenetische
Skizze, 35,
Neweastle-on-Tyne. Transactions of the North of England Institute
of Mining Engineers. Vol. xix. 1869-70. “poe
N. R. Griffith —On the Flintshire Cannel Seam, 75.
T. J. Bewick.—On the Mountain or Carboniferous Limestone Dis-
trict of the North of England, 92.
J. Rutherford.—The Coal-Fields of Nova Scotia, 1138.
A. Ross.—On Boring against Water in Coal Mines, 171.
J. Marley.—On the Magnetic Ironstone of Rosedale Abbey, Cleve-
land, 193, ;
Paris. Annales des Mines. Sixiéme Série. Tome xvii, 1870,
Delesse et de Lapparent.—Extraits de Géologie, 37.
Mussy.—Ressources Minérales de l’Ariége, 237, 459.
J. coon ole Géologiques sur l’Océanie, les iles Tahiti et Rapa,
377,
. Revue des Cours Scientifiyues de la France et de ’Htranger,
Septieme Année. ~ Nos. 51 & 52.
H. Moseley.—Théorie de la Descente des Glaciers, 806.
J. W. Dawson.—La, végétation primitive du globe, 810.
Penzance. Transactions of the Geological Society of Cornwall.
Vol. viii. Parts 1 & 2.
W. J. Henwood.—On Metalliferous Deposits and Subterranean Tem-
perature, 1,
Pest. Magyar Tudom. Akadémiai Almanach 1869-70.
——. Ertekezések a Természettudomdnyi osztély Kérébol. 1868-
' 69, parts 13 to 19.
——. -——1. .1870, parts 1: & 2.
Ertekezések a Mathematikai osztdly Korébél kiadja a M.
Tudményos Akadémia. 1868-69, parts 3-5. ee
556 DONATIONS,
Pest. A Magyar Tudomdnyos Akadémia. Ertesitdje. 1868. Nos.
9-20.
—. -——. ——,. 1869. Nos. 1-20.
—-. —-, ——. 1870. Nos. 1-12.
—. -——. Evkényvei, xiii. Parts 1&4. 1869-70.
: . Mathematikai és Természettudomdanyi Allando Bizott-
‘saga Kozlemények Vonatkozdlag a hazai viszonyokra, 1867.
V. kotet.
J. Bernith.—Magyarorsziei Asyanyok Elemzése (Chemical analysis
of some Minerals , of Hungary), 133,
J. Neubauer. Az Asatag Diatomacedk (Oszlékafélék.) Rhyolith
Csiszpalaban s Egyéb Kozetekben (The fossil Diatomacese in
Rhyolitic Tripoli and other rocks), 183 (4 plates).
Philadelphia. Proceedings of the Academy of Natural Sciences of
Philadelphia. 1870.
F. G. Meek.—Descriptions of the Fossils collected by the U.S.
Geological Survey under the charge of Clarence King, 56.
and A, H. Worthen.—Descriptions of New Species and Genera
of Fossils from the Paleozoic rocks of the Western States, 22,
Sl, Ieevarid, INOS BEG,
F, B. Meek.—Description of New Species of Invertebrate Fossils
from the Carboniferous and Devonian Rocks of Ohio, 57.
—_——,
Photographic Journal. Nos, 224-226, April to June 1871,
Quarterly Journal of Science. No. 30. April 1871.
Quekett Microscopical Club. Journal. No, 14. April 1871.
Royal Agricultural Society of England. Journal, 2nd series.
Vol. vii. Part 1.
W. C. Spooner.—On the Agricultural Capabilities of the New Forest,
220
W. Topley.—On the Comparative Agriculture of England and
Wales, 268.
Royal Cornwall and Polytechnic Society. The Thirty-cighth Annual
Report. 1870.
N. Bryant.—On the Perran Iron Lode, 98,
R. Hancock.—On the Mineral Deposits of the Old Wheal Vor Mine,
Breage, 101.
Royal Geographical Society. Proceedings. Vol. xy. No. 1. March
Sql.
Royal Institution of Great Britain. Proceedings. Vol. vi. Part 3.
DONATIONS, ' . Sai
Royal Society. Philosophcal Transactions. Vol. clix. Part 2,
1869.
O. Heer.—Contributions to the Fossil Flora of North Greenland,
being a Description of the Plants collected by Mr, Edward
Whymper during the Summer of 1867, 445 (8 plates).
R. Owen.—Description of the Cavern of Bruniquel, and its Organic
Contents (4 plates). Part I. Human Remains, 517, Part IL.
Equine Remains, 535.
. OnFossil Remains of Equines from Central and South America,
referable to Equus conversidens, Ow., Equus tau, Ow., and Equus
arcidens, Ow., 559 (2 plates).
P. M. Duncan and H. M. Jenkins.—On Paleocoryne, a Genus of
Tubularine Hydrozoa from the Carboniferous Formation, 693
(1 plate).
Vol. clx. 1870.
R. Owen.—On the Remains of a large extinct Llama (Palauchenia
magna, ee from Quaternary Deposits in the Valley of Mexico,
65 (4 plates).
——. On the Molar Teeth, Lower Jaw, of Macrauchenia patachonica,
Ow., 79 (1 plate).
N. Story-Maskelyne.—On the Mineral Constituents of Meteorites,
189 (2 plates).
G. Gore.—On Fluoride of Silver, 227.
Rh. Owen.—On the Fossil Mammals of Australia. Part III, Dipro-
todon australis, Ow., 519 (15 plates).
—. Proceedings. Vol. xix. Nos. 127 &128.
P. M. Duncan.—On the Structure and Affinities of Guynia annulata,
Dune., with Remarks upon the Persistence of Paleeozoic Types of
Madreporaria, 450.
A. Schrauf.—On the Molybdates and Vanadates of Lead, and on a
new Mineral from Leadhills, 451.
————
°
Society of Arts. Journal. 117th Session. Vol. xix. Nos. 957-969.
Tasmania, Monthly Notices of Papers and Proceedings of the Royal
Society of Tasmania. 1868,
1869.
T. Stephens.—Remarks on the Geological Structure of Part of the
North Coast of Tasmania, with special reference to the Tertiary
Marine Beds near Table Cape, 17.
—. Notes on the Occurrence of Gold at Port Cygnet, 55.
—————
e
Vienna. Anzeiger der k.-k. Akademie der Wissenschaften in Wien.
1871, Nos. 7-18.
Jahrbuch der k.-k. geologischen Reichsanstalt. Band xx.
No. 4. October to December 1870.
F, v. Hauer.—Geologische Uebersichtskarte der dsterreichisch-
ungarischen Monarchie, 463,
C. L. Griesbach.—Geologischer Durchschnitt durch Siidafrica, 501
(plate).
558
DONATIONS,
Vienna, Jahrbuch der k.-k. geologischen Reichsanstalt. Band xx.
No. 4 (continued).
C. v. Beust.—Ueber die Erzlagerstiitte vom Schneeberg unweit
Sterzing in Tirol, 505.
——. Ueber den Dimorphismus in der Geologie der Erzlagerstiatten,
513.
A. E. Reuss.—Zwei neue Pseudomorphosen, 519.
K. Hofmann.—Das Kohlenbecken des Zsilz-Thales in Siebenbiirgen,
523. r
-‘T. Fuchs.—Beitriige zur Kenntniss fossiler Binnenfaunen. IV. und
V. Die Fauna der Congerienschichten yon Tihany und Kup in
Ungarn, 531 (3 plates).
M. Neumayr.—Jurastudien, 549 (plate).
K. v. Hauer.—Das Erzrevier bei Beslinac nachst Tergove in der
Militiirgrenze, 559.
E. Tietze.—Geologische Notizen aus dem nordostlichen Serbien, 567.
Verhandlungen der k.-k. geologischen Reichsanstalt. 1871,
Nos. 4-8,
K. v. Fritsch.—Fossile Pflanzen aus dem Septarienthon, 53.
_A. de Zigno.—Fossile Pflanzen aus Marmorschichten im Venetia-
nischen, 54.
F. Simony.—See-Erosionsformen an Ufergesteien, 55.
P. G. Hauenschild.—Die Saliner-Mulde von Windischgarsten, 56.
F. Posepny.—Ueber Hohlen- und Hohlraum-Bildung, 58.
K. Paul.—Die Umgebungen von Semlin und Pancsowa in der Mili-
taregrenze, 62. . i iGe
F. Foetterle-—Weitere Notizen iiber das Vorkommen der Kalisalze
zu Kalusz in Galizien, 65.
J. Stingl— Analyse eines Schlammes aus den Opalgruben yon Ozer-
venitza bei Eperies in Ungarn, 73.
T. Fuchs.—Ueber Stérungen in den Tertiarbildungen des Wiener
Beckens, 74. 2
H. Wolf.—Brunnenprofile im Wiener Bahnhofe der Kaiserin Elisa-
beth-Westbahn, 74.
K. M. Paul.—Der nordliche Theil der Kohlenmulde der “neuen
Welt ” bei Wiener-Neustadt, 77.
. E. Tietze—Ueber ein Vorkommen yon Aptienmergeln bei Swinitza
im Banat, 78. :
T. Petersen.—Mineralogische Mittheilungen, 88.
H. Wieser.—Analyse eines Feldspathes von Blansko in Mahren,
39
H. Wolf.—Ueber den Lago d’Ansanto in der Provinz Principato
Ulteriore des ehemaligen Konigreiches Neapel, 90.
F, Karrer.—Ueber das Verhaltniss des marinen Tegels zum Leytha-
kalke, 92.
F. Posepny’.— Ueber die Glammgesteine Siebenbiirgens, 93..
——. Ueber typhonische Gesteinsmassen, 94. |
K. Peters—Ueber eine Mineralquelle in Hengsberg bei Preding,
Sy en Graz. Saugethierreste aus der Braunkohle von Voits-
erg, 107.
F. Stoliczka.—Geologische Arbeiten in Indien, 109.
J. Pauer.—Ueber den Neusiedler See, 110.
H. Wieser.—Analyse eines bitumenreichen Kalkmergels von der
neuen Jodquelle in Hall, 111.
» Analyse eines Kieselzinkerzes, 112.
DONATIONS. 559
Vienna. Verhandlungen dér k.-k. geologischen Reichsanstalt. 1871,
Nos. 4-8 (continued). ;
F, C. Clar.—Vorliufige Mittheilung tiber die Gliederung des Hoch-
lautschzuges, 113. é
A. Bauer.—Zur Kenntniss des steierischen Graphites, 114,
H. Wolf.—Ueber den steierischen Graphit, 115.
F, Karrer.—Ueber. Parkeria und Loftusia, zwei riesige Typen von
kieseligen Foraminiferen, 117. ry MS 5
. Der neue Hinschnitt an der Strasse von Ober- nach Unter-
Dobling, 117.
F, Foetterle—Vorlage der geologischen Detailkarte der Gegend
zwischen Weisskirchen, Baziasch und Moldova im serbischbanater
Militargrenz-~Regimente, 118.
E. v. Mojsisovics.—Ueber das Belemnitiden-Geschlecht Aulacoceras,
F, v. Hauer, 119. :
——. Beitrige zur topischen Geologie der Alpen, 119.
C. W. Giimbel.—Ueber Dactylopora, 127.
F. J. Pick.—Ueber die letzten Erdbeben, dann Thermen und Solfa-
taren auf Milo, 128.
H. Wieser.—Analyse des Kieserites vom Hallstatter Salzberge, 180.
. Analyse der Ausbliihungen vom Lago d’Ansanto in der Provinz
Principato Ulteriore des ehemaligen Konigreiches Neapel, 131.
M. vy. Lill—Ullmannit vom Rinkenberge in Karnten, 181.
J. pee runes Salers von Gams bei Hieflau in Steiermark,
32.
F. Babanek.—Die Erzfuhrung der Pribramer Sandsteine und Schie-
fer in ihrem Verhiltnisse zu Dislocationen, 133.
H. Behrens.—Mikroskopische Untersuchung des Pechsteins von
Cabitz, 133.
Ei. Suess.—Ueben die tertiaren Landfaunen Mittel-Italien’s, 133.
F, Schwackhofer.—Phosphorit-Vorkommen an den Ufern des Dnie-
sters, 135.
J. Nachten.—Ueber Verdriickungen und Verwiirfe der Griinbacher
Kohlenflotze, 135.
G. Stache.—Die Unghvarer Klippen, 185,
II. PERIODICALS PURCHASED FOR THE LIBRARY.
Annales des Sciences Naturelles. 5° Série. Tome xiv. No. 1,
July 1870.
E, Filhol et H. ee des. ossements de Felis spelea
découverts dans la caverne de Lherm (Ariége), Article No. 4.
Annals and Magazine of Natural History. Fourth Series. Vol. vii.
Nos. 40-42, April to June 1871,
H. G. Seeley.—Note on Prof. Cope’s Interpretation of the Ichthyo-
2 pone Head, 266. oe
. Hopkinson.—On a Specimen of Diplograpsus pristis with Repro-
ductive Capsules, 317 ‘ ai adgiale al
J. W. Dawson.—On Spore-cases in Corals, 321,
560 * DONATIONS.
Annals and Magazine of Natural History. Fourth Series, Vol. vii.
Nos. 40-42. April to June 1871 (continued).
A. Bell.—Contributions to the Crag-Fauna. Part ii., 351.
J. D. Dana.—On the supposed Legs of the Trilobite ‘Asaphus platy-=
cephalus, 366,
H. G. Seeley.—Note on the Ichthyosaurian Head, 388.
HE. Beyrich.—On the Base (Pelvis) of the Crinotdea brachiata, 393.
Freiberg. Beitriige zur geognostischen Kenntniss des Erzgebirges.
Heft 1. Die Granite von Geyer und Ehrenfriedersdorf sowie die
Zinnerzlagerstitten von Geyer. Von A. W. Stelzner. 1865.
Paleontographica: herausgegeben von Dr. W. Dunker und Dr. K.
A. Zittel. Band xix. Lief. 6.
Prof. Schenk.—Beitrage zur Flora der Vorwelt: die fossile Flora der
nordwestdeutschen Wealdenformation, 227 (7 plates).
Band xx. Lief. 1.
H. B, Geinitz,—Das Elbthalgebirge in Sachsen, 1 (10 plates).
e
—<$_—_—
°
JII. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.
Barry, A. <A Trip to the Diamond Fields. 8yvo. 1871. Presented
by Prof. J. Tennant, F.G.S.
Bell, A. Contributions to the Crag-Fauna. Part. 8vo. 1871.
Bellucci, G. Avanzidell’ Epoca Preistorica dell’ Uomo nel Territorio
di Terni. 8vo. Milano, 1870.
Bland, T. Notes relating to the Physical Geography and Geology
of, and the Distribution of Terrestrial Mollusca in certain of the
West-India Islands. 8vo. 1871.
Carpenter, W. B., and J. Gwyn Jeffreys. Report on Deep-Sea
Researches carried on during the months of July to September
1870. 8yvo. 1870. Presented by the Reporters.
Clarke, W. B. On the Progress of Gold Discovery in Australasia
from 1860 to 1871. 8vo. 1871.
———. Remarks on the Sedimentary Formations of New South
Wales. 8vo. 1870.
Czjzek, J. Erliuterungen zur geognostischen Karte der Umgebun-
gen Wiens. S8yo, Wien, 1849, Presented by Sur C. Lyell, Bart.
DONATIONS. 561
Davidson, Thomas. Sketch of the Scientific Life of. Presented by
H. Woodward, Hsq., F.GS.
Dana, J. D. On the supposed Legs of the Trilobite, “ Asaphus
platycepalus.” 8yo. 1871.
Denny, H. On the Former Existence of the Roebuck in the West
Riding of Yorkshire. Presented by Sur C. Lyell, Bart.
De Rance, C. E. Map showing the Tract traversed by the Earth-
Waves of the 17th, 18th, and 22nd of March 1871, in the six
Northern Counties of England.
——, On the two Glaciations of the Lake-District. Svo. 1871.
Dublin University Magazine, for April 1871. Presented by H.
Pearce, Esq., F.GS.
Enys, J. S. Remarks on the Intensity and Quantity of the Junction
Changes of Sussex and Cornwall, considered as Mining Districts.
8vo. 1863. Presented by the Rev. W. Whitaker, Esq., F.GS.
Falconer, W. Dissertation on St. Paul’s Voyage. 2nd edition. 8vo.
1870. Presented by T. Falconer, Esq., F.G.S.
Favre, H. Etudes sur la Géologie des Alpes. 8vo. Genéve et Bale,
1870.
Revue des Travaux relatifs 4 la Géologie et 4 la Paléontolo-
gie de la Suisse, pendant l’année 1869. 8vo. Genéve, 1870.
Geologische Specialkarte des Grossherzogthums Hessen und der an-
grenzenden Landesgebiete. Section Bladenbach, von R. Ludwig
(with explanation). Darmstadt, 1870. From the Geological So-
ciety of the Middle Rhine.
Geology, The Science of. 12mo. Glasgow, 1839. Presented by W.
Whitaker, Esq., F.GS.
Guiscardi, G. Sopra un Teschio Fossile di Foca. 4to. Napoli,
1871.
Gutbier, L. v. Karte der Dresdner Haide; mit geologische Erlau-
terungen. 8vo. Dresden, 1865. Presented by Sir C. Lyell, Bart.
Haast, J. Moas.and Moa Hunters. Anniversary Address delivered
at the Philosophical Institute of Canterbury. 8vo. 1871.
Heer, O. Die miocene Flora und Fauna Spitzbergens. 4to. Stock-
holm, 1870.
Helmersen, G. v. Die Geologie in Russland. Presented by Sir C.
Lyell, Bart.
Helmersen, Gv. Notiz iiber die Berge Ak-tau und Kara-tau auf
der Halbinsel Mangyschlak, am Ostufer des Kaspischen Meeres.
8vo, St. Petersburg, 1870.
562 DONATIONS.
Helmersen, G.v. Ueber die Braunkohlenlager bei Smela im Gouyerne-
ment Kjew und bei Jelisawetgrad im Gouvernement Cherson.
8vo. St. Petersburg, 1869.
Hopkinson, J. Ona Specimen of Diplograpsus pristis with Renee
ductive Capsules. Syo. 1871.
Hull, E. On the Age of the Ballycastle Coal Field. S8yo. 1871.
Kirkby, J. W., and J. Duff. Notes on the Geology of Part of South
Durham. 8vo. 1871.
Lindstrém, G. A Description of the Anthozoa Perforata of Gotland.
Ato. Stockholm, 1870.
Mackay, A. A Visit to Sydney and the Cudgegong Diamond Mines.
Svo. Melbourne, 1870.
Mallet, F. R. On the Geological Structure of the Country near Ader.
with reference to the practicability of sinking Artesian Wells.
(Memoirs of the Geological Survey of India, “vol. vii. part 3.)
Presented by Sir C. Lyell, Bart.
Marcou, J. De la Science en France. Premicre Partie. aro,
Paris, 1869.
. Les derniers travaux sur le Dyas et Trias de Russie, Syvo.
Paris, 1869.
Notice Biographique sur M. Auguste Dollfus-Gros. 8vo.
Paris, 1869.
Notes pour servir 4 Vhistoire des anciens glaciers de l’Au-
vergne. 8yo. Paris, 1869.
Note sur une météorite tombée le 11 Juillet 1868, 4 JESSIE,
_ prés Ornans (Doubs). Syo. Paris, 1868. :
Markham, C. R. A Memoir on the Indian Surveys. S8yvo. 1871.
Marsh, O. C. Descriptions of some New Fossil Serpénts from the
Tertiary Deposits of Wyoming. 8vo. 1871.
——. Notice of a Fossil Forest in the Tertiary of California. 8vo.
1871.
——. On the Geology of the Eastern Uintah Mountains, 8vo.
1870. ;
Murchison, R. I. Address at the Anniversary Meeting of the Royal
Geographical Society, 22nd May, 1871.
Naumann, C.F. Elemente der Mineralogie. S8yvo. Leipzig, 1871.
Ortlieb, J., et H. Chellonneiw. Etude Géologique des Collines Ter-
_ tiaires du Département du Nord comparées avec celles de la Bel-
gique. 8vo. Lille, 1870.
>)
DONATIONS. 563
Reinwarth, C. Ueber die Steinsalzablagerung bei Stassfurt und die
dortige Kali-Industrie, sowie tiber die Bedeutung derselben fiir
Gewerbe und Landwirthschaft. 8yo. Dresden, 1871,
Report of the Chief Commissioner of Mines for the Province of Nova
Scotia, for the year 1870. 8yvo. Halifax, N.S., 1871. . Krom the
Government of Nova Scotia.
Report. The Ninth Annual Report of the Free-Libraries Committee.
Birmingham, 1870. . Presented by the Committee.
Roemer, F. Geologie von Oberschlesien. Text, Atlas, Maps, and
Profiles. S8yo. Breslau, 1870.
Rowlandson, T. A Treatise on Earthquake Dangers, Causes, and
Palhatives. 8yvo. San Francisco, 1869.
Royal Commission on Water Supply. Minutes of Evidence taken
before the Commissioners, February to December 1868. Fol.
London, 1869. From the Commissioners. f
. Appendix to the Minutes of Evidence, together with Maps
and Plans, and an Index. Fol. London, 1869. From the Com-
MAssioners.
Report of the Commissioners. Fol. London, 1869. From
the Commissioners.
Royal Society of New South Wales. Address delivered at the Anni-
versary Meeting, 25th May, 1870; with a Postscript, by the Rev.
W.B. Clarke. 8yo. Sydney, 1871. Presented by the Rev.W. B.
Clarke, M.A.
Sandberger, F. Die Land- und Siisswasser-Conchylien der Vorwelt.
Ato. Wiesbaden, 1870.
Studer, B. Zur Geologie des Ralligergebirges. 8vo. 1871.
Sveriges Geologiska Undersékning. Sheets Nos. 36-41 and expla-
nations. From the Swedish Geological Commission.
Wilhamson, R. 8. On the use of the Barometer on Surveys and
Reconnaissances. (With an Appendix.) 4to. New York, 1868.
Presented by Sir C. Lyell, Bart.
Victoria. Mineral Statistics of Victoria. From the Colonial Govern-
ment, Victoria.
Reports of the Mining Surveyors and Registrars. Quarter
ending 31st December 1870. From the Colonial Government,
Victoria.
564 DONATIONS.
IV. BOOKS &c. PURCHASED FOR THE LIBRARY.
Bayan, F. Mollusques Tertiaires. 4to. Paris, 1870.
Erdmann, A. Exposé des Formations Quaternaires de la Suede.
Text, 8vo; Atlas, 4to. Stockholm, 1868.
Fraas, O. Die Fauna von Steinheim. 4to. Stuttgart, 1870.
Naumann, C.F. Elemente der Mineralogie. 8yo. Leipzig, 1871.
Roemer, F. Geologie von Oberschlesien. Two vols., with Sections
and Map by O. Degenhardt. 8yo. Breslau, 1870.
Wiess, C. E. Fossile Flora der jiingsten Steinkohlenformation und
des Rothliegenden im Saar-Rhein-Gebiete. Zweites Heft. 4to.
Bonn, 1871.
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.]
Addo Drift, 503.
Africa, South, Cretaceous rocks of, 60.
, Mr. C, L. Griesbach on
the geology of Natal, in, 53.
: , Mr. G. W. Stow on the
geology of, 497, 523; Jurassic for-
mations of, 497; Posttertiary for-
mations of, 515; Dicynodon-forma-
tion of, 523; climatal changes and
cag "denudation of, 534.
, remarks on some speci-
mens from, by Dr. George Grey, 49.
Age of the Nubian Sandstone, 404.
Agnostus cambrensis, 400.
Albany, Lower, section through, 537.
: , Specimens from the Car-
boniferous rocks of, 50.
Aldborough, section in ballast-pit at,
335; fossils from the Red Crag
near, 332; fossils from Thorpe-pit
near, 340.
Aldeby, section in pit at, 454; fossils
from, 455.
Alexandria, section from, to the Orange
River, 537.
Allophane, Mr. W. D. Herman on,
and an allied mineral found at
~ Northampton, 234.
Am-Ende-der-Welt, 314.
Ammonites Kayet, 63.
rembda, 63.
umbolazi, 63.
Amsterdam Flats, section through,
515.
Analysis of allophane and an allied
mineral, 236; of harmotome, 374.
Anamesite veins in Higg, 299.
Anamesites of the island of Higg, 290.
Andrie’s Neck, sketch from, 547.
VOL. XXYII.
Anisoceras rugatum, 63.
Anniversary Address of the President,
xxx-lxxy, See also Prestwich, Jos.,
sq.
Antequera, plain of, 111.
Arca capensis, 66.
Asia, Hastern, and North China, Mr.
T. W. Kingsmill on the probable
origin of deposits of ‘ Loess” in,
376.
Auchindoun Castle, section through,
102.
Bacton, section in cliff near, 464.
Banfishire, Mr. T. F. Jamieson on the
older metamorphic rocks and gra-
nite of, 101.
Barnes series of the Punfield forma-
tion, 218.
Basalt plateau of the island of Higg,
290.
Basalt veins in Higg, 299.
Bath district, Mr. W. Stephen Mitchell
on the denudation of the Oolites of
the, with a theory on the denudation
of Oolites generally, 228.
Bawdsey Cliff, sections in, 327, 334;
fossils from the Red Crag of, 337.
Beaches, raised, in South Africa,
517.
Bear Island, Prof. O. Heer on the
Carboniferous flora of, 1.
Beer Head, diagram of upper part of
cliff west of, 98.
Beinn Bhuidh, section through, 287.
Ben Aigan, section through, 102.
Bethelsdorp saltpan, 506.
Bideann Boidheach, Eigg, section of
the cliff of; 308.
a
INDEX TO THE PROCEEDINGS.
Bishopford Bridge, Norwich, section
in pit at, 469.
Bluff, Port Natal, section from, to the
Rooy-kop, 59.
Boharm, section through, 102.
* Bone-bed,” Dr. F. Royston Fairbank
on the discovery of a, in the lowest
of the “‘ Lynton Grey-Beds,” North
Devon (title only), 33.
Bongolo valley, 541.
Bonney, Rey. T. G., on the formation
of “cirques,” and their bearing
upon theories attributing the exca-
vation of Alpine valleys mainly to
the action of glaciers, 312.
re intrusive, in the island of Hige,
294.
Bottra’s hill, section through, 537.
Boulders of greenstone &e. imbedded
in clay and grit, Karoo formation,
Natal, 58.
Bramerton, fossils from, 457.
Branscombe Mouth, section of part
if of the top of the cliff west of,
Breccias of the island of Higg, 293.
Brewsterite, 373.
Britain, Mr. W. B. Dawkins on the
discovery of the Glutton in, 406.
British Guiana, Mr. J. G. Sawkins on
the geology of, 419.
British Islands, Prof. A. Geikie on
the Tertiary volcanic rocks of the,
279.
Prete Bay, Punfield formation in,
Brodie, Rev. P. B., on the “ passage-
beds” in the neighbourhood of Wool-
hope, Herefordshire, and on the
discovery of a new species of Hury-
pterus and some new land-plants
in them, 256.
Brooke, Isle of Wight, Mr. J. W.
Hulke on a large reptilian skull
from, probably Dinosaurian, and
referable to the genus Jguanodon,
1199:
Broom hill, near Orford, section of a
pit on, 122; fossils from the Coral-
line Crag of, 123.
Bryozoa of the Coralline Crag of Suf-
folk, 128.
Buffel-Doorns flat, 541; section show-
ing outlets from, 542; section show-
ing the successive outlets on the 8.
an S.H. sides of, 542.
Bulchamp, section in pit near, 344;
fossils from, 344.
Burghersdorp, section through, 537.
Butley Abbey, section in a pit near,
829 ; fossils from the Red Crag near,
330.
Calamites, Sigillaria, and Calameden-
dron, Dr. J. W. Dawson on the
structure and affinities of, 147.
Calamites, structure of, 158.
Calamodendron, Sigillaria, and Cala-
mites, Dr. J. W. Dawson on the
structure and affinities of, 147.
Calamodendron, structure of, 155.
Calcite, 373, 374.
Cambrian rocks, Lower, of St. David’s
promontory, table of the, 391; com-
parison of the fossils of, with those
of other parts of the world, 391—
398; table of fossils from, 396.
Canuku mountains, section through,
421,
Cape of Good Hope, Mr. G. Gilfillan
on the diamond-districts of the,
72.
Carboniferous flora of Bear Island,
Prof. O. Heer on the, 1. ;
Carboniferous rocks of Lower Albany,
specimens from the, 50.
Cardium denticulatum, 67.
Carenacru, section through, 421.
Carpolites umbonatus, 444, 446.
Carruthers, William, Hsq., on some
supposed vegetable fossils, 443.
Caryophyllia cylindracea, Prof. Dun-
can on the persistence of, in the
Coral fauna of the deep sea, 484,
Caulopteris antiqua, 271.
Lockwoodi, 270.
(Protopteris) peregrina, 272.
Cephalopoda of South-African and
Indian Cretaceous rocks, 64.
Cerithium (Fibula?) detectum, 64.
kaffrarium, 64.
Chalk of the southern part of Dorset
and Devon, Mr. W. Whitaker on
the, 93.
of the cliffs from Seaford to Hast-
bourne, Sussex, Mr. W. Whitaker
on the (title only), 92.
Chemnitzia undosa, 65.
Chillesford, sections at, 386, 3373
fossils from, 331, 337.
Chillesford series, 386-339, 343-345.
Chimeroid fish, Sir P. G. Hgerton
on a new, from the Lias of Lyme
“Regis, 275.
China, North, and Hastern Asia, Mr.
T. W. Kingsmill on the probable
origin of deposits of “ Loess” im,
376.
——, ——, evidence of late depression
; in, 378.
INDEX TO THE PROCEEDINGS.
Chlor ite-slate formation of Natal, 55.
Cirques, Rev. T, G. Bonney on the
formation of, and their bearing upon
theories attributing the excavation
of Alpine valleys mainly to the
action of glaciers, 312.
Cirripedes of the Coralline Crag of
Suffolk, 130.
Clay-slate formation of Natal, 55.
Clegyr valley, section across, 388.
Climatal changes of South Africa, Mr.
G. W. Stow on the, 534.
Coal-bearing strata of Eastern Spain,
224.
Coal from the Stormberg range, 51.
—— in Natal, 70.
Coltishall, section in chalk-pit at, 459 ;
fossils from, 459.
Compton Bay, Punfield formation in,
219.
Conewyatchi river, section across,
421.
Conocoryphe Lyellit, 399.
solvensis, 400.
Continent, Southern, on the probable
existence of a, 546.
Contour-plan of exposures of strata on
the Upper Zwart Kei, 527.
Copper in Natal, 70.
Coral, Prof. Duncan on a new species
of, from the Red Crag of Walding-
field, 369.
Coralline Crag of Suffolk, Mr. J.
Prestwich on the, 116; fossils of
a 125, 137 ; general section of the,
21,
Corals of the Coralline Crag of Suf-
folk, 131.
Cotinga river, section across, 421,
Cowleaze series of the Punfield for-
mation, 218.
Cradock, Cape Colony,
from, 49.
Crag-beds of Suffolk and Norfolk, Mr.
J. Prestwich on the structure of the,
with some observations on their or-
ganic remains.—Part I. The Coral-
line Crag of Suffolk, 116.
specimens
of Hssex and Suffolk, 325.
. Part III. The Norwich
Crag and Westleton beds, 452.
Crag, Coralline, Mollusca from the,
494,
‘ , of Suffolk, Mr. J. Prest-
wich on the, 116; fossils of the,
Va 137; general section of the,
21,
Crag, Norwich, Mr. J. Prestwich on
the, 452,
Part II. The Red Crag-
Crag, Red, of Hssex and Suffolk, 325.
——s , of Waldringfield, Prof
Duncan on a new species of Coral.
from the, 569.
Cretaceous and Neocomian, uncon-
formity of the, in the south of Eng-
land, 221.
Cretaceous, Neocomian, and Wealden
of the south of England, relations:
of the Punfield formation to the,
221.
Cretaceous rocks of South Africa, 60.
Cretaceous series of South Africa and
India compared, 68.
Cretaceous, variation in character of
the, from east to west, in the south
of England, 221.
Creux de Champs, 312.
Creux du Vent, 313.
Crocodilus gaudensis, 30.
Croda Malcora, 313. j
Crustacea of the Coralline Crag of
Suffolk, 130.
Crustaceans, Mr. H. Woodward on
some new, from the Lower Hocene_
of Portsmouth, 90.
Cumparuyama river, section across,
421.
Cuyler Manor, section at, 498, 499.
Cystoseirites nutans, 447.
Dawkins, W. Boyd, Esq., on the dis-
_covery of the Glutton ( Gulo luscus)
in Britain, 406.
Dawson, Dr. J. W., on new tree-ferns
and other fossils from the Devonian,
269.
==, , on the structure and af-
finities of Sigillaria, Calamites, and
Calamodendron, 147.
Denudation, glacial, of South Africa,
Mr. G. W. Stow on the, 534.
of the Oolites of the Bath district,
Mr. W. Stephen Mitchell on the,
with a theory on the denudation of
Oolites generally, 228.
Deveron, section from the Spey to the,
- 102,
Devon, North, Dr. F. Royston Fairbank
on the discovery of a;‘‘ bone-bed” in
the lowest of the Lynton grey-beds,
(title only), 33.
and Dorset, Mr. W. Whitaker
on the chalk of the southern part of,
93.
Devonian, Dr. J. W. Dawson on new
tree-ferns and other fossils from the,
269.
Diadema, 67.
Diamond-districts of the Cape of,
INDEX TO THE PROCEEDINGS.
Good Hope, Mr. G. Gilfillan on
the, 72.
Dieppe, Mr. W. Whitaker on the cliff-
sections of the Tertiary beds west of,
263.
Dinosaurian skull, Mr. J. W. Hulke
ona probable, from Brooke, Isle of
Wight, 199.
Dip of the saliferous beds of the
Uitenhage formation, 511.
Distribution, stratigraphical, of the
British fossil Lamellibranchiata,
Mr. J. L. Lobley on the, 411.
Dolerites of the island of Higg, 290.
Dolerite veins in Higg, 299.
Donations to the library, viii, 34, 162,
357, 549; museum, vii.
Donegal, Mr. A. H. Green on the geo-
logy of part of the county of, 449.
Dordrecht, section at, 524; section
through, 537.
Dorset, Mr. J. W. Hulke on a frag-
ment of a Teleosaurian snout from
Kimmeridge Bay, 442.
—, Mr. J. W. Hulke on an Ichthyo-
saurus from Kimmeridge Bay, 440.
and Devon, Mr. W. Whitaker
on the chalk of the southern part
of, 98.
Drayson, Lieut.-Col., on the probable
cause, date, and duration of the
Glacial epoch of geology, 232.
Dunan Thalasgair, section through,
287.
Dunean, Prof. P. Martin on a new
species of coral from the Red Crag
of Waldringfield, 369.
——, on the persistence of Caryophyl-
lia cylindracea, Reuss, sp., a Creta-
ceous species of coral in the coral
fauna of the deep sea, 434.
Durban, section through, 59.
Durdle Cove, section of chalk with
flints in eastern side of, 95.
Dykes in the island of Higg, 298.
Hastbourne, Sussex, Mr. W. Whitaker
on the chalk of the cliffs from Sea-
ford to (title only), 92.
Haston Bavent cliff, section near north
end of, 462; section of cliff at, 345;
fossils from the crag and Chilles-
ford clay at, 345.
Hehinodermata of the Coralline Crag
of Suffolk, 131.
Heonomic geology of Natal, 70.
Egerton, Sir P. G., on a new Chime-
roid fish from the Lias of Lyme Regis
(Ischyodus orthorhinus 8 ), 275.
~Heggs, fossil, 446.
Bigg, geology of the island of, 285;
map of, 286 ; section of, 287; Oolitic
series of, 288; volcanic series of,
289; Scur of, 303.
Eland’s Post, section through, 537;
table of elevations from, to the banks
of the Orange river, near Aliwal,
548.
Elevations, table of, from Hland’s Post
to the banks of the Orange River,
near Aliwal, 548.
Engelberg, cirque near, 323.
Entomostraca of the Coralline Crag of
Suffolk, 130.
Eurypterus Brodiei, 262.
Eurypterus, Rey. P. B. Brodie on the
discovery of a new species of, in the
“‘passage-beds” in the neighbour-
hood of Woolhope, Herefordshire,
256.
—, Mr. H. Woodward on a new
species of (H. Brodiei) from Perton,
near Stoke Hdith, Herefordshire,261.
Fairbank, Dr. F. Royston, on the dis-
covery of a ‘“‘bone-bed” in the
lowest of the ‘Lynton Grey-beds,”
North Devon (title only), 33.
Fauna of the Izinhluzabalungu depo-
sits, 62.
Felstone vein in Higg, 299.
Fer-a-Cheval, 312.
Ferns, tree, Dr. J. W. Dawson on new,
and other fossils from the Devonian,
269.
Fish, Sir P. G. Egerton on a new
Chimeroid, from the Lias of Lyme
Regis, 275.
Fish-remains of the Coralline Crag of
Suffolk, 132.
Flora, Carboniferous, of Bear Island,
Prof. O. Heer on the, 1. i
Fluid-casts, 445.
Foraminifera of the Coralline Crag of
Suffolk, 131.
Forest-bed of Norfolk, mammalian
remains from the, 466; plants from
the, 467.
Forest-zones of the Dicynodon forma-
tion, 523.
Fossils from South Africa, 49; from
the Devonian, 269; from the Long-
mynd rocks of St. David’s, 399;
from the Lower Eocene of Ports-
mouth, 85, 90; from the Nubian
sandstone, 405 ; from the Red Crag,
330, 331, 332, 337, 338, 339, 348,
344, 345, 346, 347, 351; of the Co-
ralline Crag of Suffolk, 125, 187;
of the saliferous beds of the Uiten-
INDEX TO THE PROCEEDINGS.
hage formation, 511 ; reptilian, from
-Gozo, Mr. J. W. Hulke on, 29;
South-African Cretaceous, 63.
Fossils, Mr. W. Carruthers on some
supposed vegetable, 443.
Gedgrave, Low, fossils from the Coral-
line Crag near, 124.
Geikie, Prof. Archibald, on the Ter-
tiary volcanic rocks of the British
Islands (first paper), 279.
Geography (physical) of Natal, 53.
Geology, economic, of Natal, 70; of
British Guiana, 419; of Donegal,
449; of St. David’s promontory,
_ 384; of the island of Higg, 285,
309.
of Natal, in South Africa, Mr.
C. L. Griesbach on the, 53.
— of South Africa, Mr. G. W. Stow
on the, 497, 523.
— of the neighbourhood of Malaga,
D. M. d’Orueta on some points in
the, 109.
Gilfillan, G., Esq., on the diamond-
districts of the Cape of Good Hope,
79
Glacial denudation of South Africa,
Mr. G. W. Stow on the, 534.
Glacial epoch of geology, Lieut.-Col.
Drayson on the probable cause, date,
and duration of the, 232. -
Glaciers, Rev. T. G. Bonney on the
theory of the excavation of alpine
valleys by, 312.
Glenmarkie hill, section through, 102.
Glutton, Mr. W. B. Dawkins, on the
discovery of the, in Britain, 406.
Gneiss, greenstone, and granite, boul-
ders of, imbedded in clay and grit,
Karoo formation, Natal, 58.
Gneiss of Banffshire, 102; of Natal,
54. :
Gold in Natal, 70.
Gomer, near Low Gedgrave, fossils
from the Coralline Crag at, 124.
Gozo, Mr. J. W. Hulke, on some rep-
tilian fossils from, 29.
Grahamstown, section through, 537.
Granite, greenstone, and gneiss, boul-
ders of, imbedded in clay and grit,
Karoo formation, Natal, 58.
Granite of Banffshire, Mr. T. F. Jamie-
son on the older metamorphic rocks,
and, 101; origin pf the, 105.
of Natal, 54.
Graphite in Natal, 70.
Grassridge, section through, 515.
Gravel-deposits of the Weald, 9;
of Hampshire, 23.
Green, A. H., Hsq., on the geology
a pet of the county of Donegal,
Greenstone, granite, and gneiss, boul-
ders of, imbedded in elay and grit,
Karoo formation, Natal, 58.
Grey, Dr. George, remarks on some
specimens from South Africa, 49.
Griesbach, CO. L., Esq., on the geology
of Natal, in South Africa, 53.
Guiana, British, Mr. J. G. Sawkins on
the geology of, 419.
Guilielmites permianus, 446.
Gulo luscus, 406.
Hangklip, section of, 531; section
through, 537.
Harkness, Prof. R., and H. Hicks, Hsq.,
on the ancient rocks of the St.
David’s promontory, South Wales,
and their fossil contents, with de-
' seriptions of the new species by H.
Hicks, Hsq., 384.
Harmotome, 373, 374.
Hawkshaw, J. C., Esq., on the peat-
and underlying beds observed in
the construction of the Albert Dock,
Hull, 237.
Heer, Prof O., on the Carboniferous
flora of Bear Island, 1.
Herefordshire, Rey. P. B. Brodie on
the “passage-beds”’ in the neigh-
bourhood of Woolhope, and on the
discovery of a new species of Lury-
pterus and some new land-plants in
them, 256. i
Herman, W. Douglas, Esq., on allo-
phane, and an allied mineral found
at Northampton, 234.
Hicks, Henry, Esq., and Prof. R. Hark-
ness on the ancient rocks of the St.
David’s promontory, South Wales,
and their fossil contents, with de-
scriptions of the new species, by H.
Hicks, Esq., 384,
Hulke, J. W., Esq., note on a large
reptilian skull from Brooke, Isle
of Wight, probably Dinosaurian, and
referable to the genus Jguanodon,
199.
, on a fragment of a Teleosaurian
snoutfrom Kimmeridge Bay, Dorset,
442,
, on an Ichthyosaurus (L. enthe-
kiodon), from Kimmeridge Bay,
Dorset, 440.
——, on some reptilian fossils from
Gozo, 29.
Hull, Mr. J. C. Hawkshaw on the
peat- and underlying beds observed *
INDEX TO THE PROCEEDINGS.
in the construction of the Albert
Dock, 237.
Ice-scratches at Reit-Poort, 8. Africa,
541
Ichthyosaurus enthekiodon, 440.
gaudensis, 29,
Ichthyosaurus, Mr. J. W. Hulke on an,
from Kimmeridge Bay, Dorset, 440.
Iguanodon, Mr. J. W. Hulke on a
skull from Brooke, Isle of Wight,
probably referable to the genus,
199.
Inanda flats, section from the coast to,
India and South Africa, comparison of
Cretaceous series in, 68.
India, Northern, Mr. 'T. Login on the
most recent geological changes of
- the rivers and plains of, 451.
Intrusive bosses, sheets, dykes, and
~ veins in the island of Hige, 294.
Ireng river, section across, 421,
Ischyodus orthorhinus, 275.
Isle of Wight, Mr. J. W. Hulke ona
large reptilian skull from Brooke,
199.
eer Punfield formation in the,
17.
—, section of the, Punfield forma-
tion in the, 213. ;
Izinhluzabalungu caves, 61; deposits,
fauna of, 62.
Jamieson, T. F., Hsq., on the older
metamorphic rocks and granite of
Banffshire, 101. 5
Jones, Prof. T. Rupert, notes on spe-
cimens from South Africa, 49-52.
Judd, J. W., Hsq., on the Punfield
» formation, 207.
une formations of South Africa,
Se
Kaffraria, British, denudation in, 543.
Kaga mountains, 543.
Karakanang valley, section across, 421.
Karoo beds, configuration and origin
of the, 535 ; denudation of the, 538 ;
formation, 523; of Natal, 57; spe-
cimens from the, 49, 50.
Katberg, 539; sections through, 537.
Kat river, sections through, 537.
Kessingland, section in cliff between,
and Pakefield, 463.
Kimmeridge Bay, Dorset, Mr. J. W.
Hulke on a fragment of a Teleosau-
rian snout from, 442.
, Mr. J. W. Hulke on an
Ichthyosaurus from, 440.
Kingsmill,'Thomas W., Esq., onthe pro-
bable origin of deposits of ‘‘ Loess”
in North China and Hastern Asia,
376.
Klaas-Smit’s river,
source of, 531.
Kloppersfontein, section through, 537.
Koega Kopjes, section through, 515.
Koega river, sandstones on the, 505;
section through the, 515.
Krantzkop mountain, section through
the, 57.
Kroome mountains, 543.
section at the
Lamellibranchiata, Mr. J. L. Lobley
on the principal features of the
stratigraphical distribution of the
British fossil, 411.
Leperditia? cambrensis, 401.
Level, Mr. J. J. Murphy on the con-
nexion of volcanic action with
changes of (Abstract), 108.
Lias, Lower, Rheetic beds, and New Red
Marl, Prof. A. C. Ramsay on the
physical relations of the, 189.
Lias, Sir P. G. Egerton, on a new Chi-
meroid fish from the, of Lyme
Regis, 275.
Lingulella primeva, 401.
Lithodomous mollusca, Sir W. C.
pane on supposed borings of,
231.
Lobley, J. Logan, Esq., on the prin-
cipal features of the stratigraphical
distribution of the British fossil
Lamellibranchiata, 411.
Loess, Mr. T. W. Kingsmill on the
probable origin of deposits of, in
North China and Hastern Asia, 376.
Login, T., Hsq., on the most recent
geological changes of the rivers and
plains of Northern India, founded
on accurate surveys and the artesian
well-boring at Umballa, to show the
practical application of Mr. Login’s
theory of the abrading and trans-
porting power of water to effect such
changes, 451.
Longmynd rocks of St. Dayid’s, fossils
from the, 399.
Lower Albany, specimens from the
Carboniferous rocks of, 50.
Lower Hocene of Portsmouth, Mr. H.
Woodward on some new crustaceans
from the, 90.
Lower Lias, Rheetic beds and New Red.
Marl, Prof. A. C.; Ramsay on the
physical relations of the, 189.
Lower Sunday’s river, sections on the,
500
INDEX TO THE PROCEEDINGS.
Lower Tertiary deposits recently ex-
posed at Portsmouth, Mr. C. J. A.
Meyer on, 74.
Lulworth Cove, 217.
Lycopodites, 274.
Lyme Regis, Sir P. G. Egerton on a
Chimeroid fish from the Lias of, 275.
Lynton Grey-beds, North Devon,
Dr. F. Royston Fairbank on the
discovery of a ‘“‘bone-bed’”’ in the
lowest of the (title only), 33.
McLoughlin’s Bluff, 500; section from
Zwartkops river to, 515.
Malaga, D. M. d’Orueta on some
points in the geology of the neigh-
bourhood of, 109.
Mammalian remains from the forest-
bed of Norfolk, 466; of the Coral-
line Crag of Suffolk, 152.
Map of the geology of British Guiana,
420; of the island of Hige, 286; of
the Newhaven Tertiary outliers,
265; showing position of sections
_at Dordrecht, on the Upper Zwart
Kei and at Klaas-Smit’s river, 531.
Metals of Natal, 70.
Metamorphic rocks and granite of
Banffshire, Mr. T. F. Jamieson on
the, 101.
Mewps Bay, 217.
Meyer, C. J. A., Hsq., on Lower Ter-
tiary deposits recently exposed at
Portsmouth, 74.
Mica-schists of Natal, 55.
Microdiscus sculptus, 400.
Minerals of Strontian, Argyllshire, Mr,
R. H. Scott on the, 372.
Mitchell, W. Stephen, Esq., on the
denudation of the Oolites of the
Bath district, with a theory on the
denudation of Oolites generally,228.
Modder-drift, 503.
Mollusca, list of, from the Red and
Norwich Crags, 480.
——,, lithodomous, Sir W. C. Tre-
velyan on supposed borings of, 231.
—— of the Coralline Crag of Suffolk,
126, 137.
Moraines of the Kathberg, 539.
Morvenite, 373.
Mundesley, section of the Westleton
beds near, 467.
Murphy, Joseph John, Hsq., on the
connexion of volcanic action with
changes of level (Abstract), 108.
Natal, South Africa, Mr. C. L. Gries-
bach on the geology of, 53.
Neocomian and Cretaceous, unconfor-
mity of the, in the south of Eng-
land, 221.
Neocomian and Wealden, thinning out
of the, in the south of England, 222.
, Cretaceous, and Wealden, of the
south of England, relations of the
Punfield formation to the, 221.
Newhaven, Mr. W. Whitaker on the
cliff-sections of the Tertiary beds at,
265. .
New Red Marl, Rhetic beds, and
Lower Lias, Prof. A. C. Ramsay on
the physical relations of the, 189.
Neggerathia gilboensis, 273.
Norfolk and Suffolk, Mr. J. Prest-
wich on the Crag-beds of, with
some observations on their organic
remains.—Part I. The Coralline
Crag of Suffolk, 115.
. Part II. The Red Crag of
Essex and Suffolk, 325.
. Part III. The Norwich
Crag and Westleton beds, 452.
Normandy, Mr. W. Whitaker on the
cliff-sections of the Tertiary beds
west of Dieppe in, 263.
Northampton, Mr. W. D. Herman on
a mineral allied to allophane found
at, 234,
Norwich, Thorpe pit, section in, 456;
fossils from, 456; Bishopford bridge,
section at, 469.
Nubian Sandstone, Mr. R. Tate on the
age of the, 404.
Old Grahamstown road, section at,
498, 499.
Old Red Sandstone, Prof. Ramsay on
the, 241,
Oolites of the Bath district, Mr. W.
Stephen Mitchell on the denuda-
tion of the, with a theory on the de-
nudation of Oolites generally, 228.
Oolithes bathonice, 447.
obtusatus, 447.
sphericus, 447.
Orange river, section from Alexan-
dria to the, 5387; table of elevations
from Eland’s Post to the banks of
the, near Aliwal, 548.
Orange valley, crystalline rocks from,
50.
Orford, section of a pit on Broom
hill, near, 122; fossils from the
- Coralline Crag near, 128.
Orueta, D. M. d’, on some points in
the geology of the neighbourhood
of Malaga, 109,
Pakefield, section in cliff between Kes-'
INDEX TO THE PROCEEDINGS.
singland and, 463; of lower part
of cliff 14 mile south of, 463.
Paleocarystes glabra, 90.
Palxontology of the Keuper, Infra-
lias, and Rheetic beds, 193.
Paradoxides Harknessi, 399.
Passage-beds in the neighbourhood of
Woolhope, Herefordshire, the Rey.
P. B. Brodie on the, and on the dis-
covery of a new species of Hury-
pterus and some new land-plants
in them, 256.
Paston cliff, section in, 465.
Peat- and underlying beds observed in
the construction of the Albert Dock,
Hull, Mr. J. C. Hawkshaw on the,
237.
Pecten amapondensis, 66.
Pectunculus africanus, 66.
Periods, succession of, in South Africa,
544.
Permian strata of England, Prof.
Ramsay on the, 245.
Perton, near Stoke Edith, Hereford-
shire, Mr. H. Woodward on a new
species of Hurypterus from, 261.
Pirara, section through, 421.
Pitchstone and porphyry coulées of the
Setr of Higg, 303.
—— filling a cavity in dolerite, Hige,
301.
; veins in Higg, 299.
Plants from the forest-bed of Norfolk,
467.
Plants, Rev. P. B. Brodie on the dis-
covery of some new land-, in the
“passage-beds” of the neighbour-
_ hood of Woolhope, Herefordshire,
256.
Pliocene or Postpliocene strata of the
_ interior of South Africa, 515; on
the coast, 516; on the coast and in-
land, 517.
Plutonia Sedgwickii, 399.
Point St. John, section from, across
St. Dayid’s promontory to Porth-y-
Rhaw, 388.
Porphyrite of the island of Hige, 292.
Porphyry and pitchstone coulées of
the Sctr of Higg, 303.
Port Elizabeth, salt vlei near, 507;
section through, 508.
Porth-y-Rhaw, section from Point St.
John to, 388.
Port Natal, section from, to the Rooy-
Kop, 59.
Portsmouth, Mr. H. Woodward on
some new crustaceans from the
Lower Eocene of, 90.
——, Mr. C. J. A. Meyer on Lower
Tertiary deposits recently exposed
at, 74.
Portsmouth, ‘sections at, 75, 79, 80,
83.
Postpliocene or Pliocene strata of the
interior of South Africa, 515; on
the coast, 516; on the coast and in-
land, 517.
Posttertiary or Tertiary strata of South
Africa, 515.
Prestwich, Joseph, Esq., on the struc-
ture of the Crag-beds of Suffolk and
Norfolk, with some observations on
their organic remains.—PartI. The
Coralline Crag of Suffolk, 115.
Part II. The Red Crag
of Hssex and Suffolk, 325.
. Part III. The Norwich
Crag and Westleton beds, 452.
Prestwich, Jos. Esq. (President),
Address on presenting the Wollas-
ton Medal to Prof. Ramsay, xxvii;
Address on presenting the balance of
the proceeds of the Wollaston dona-
tion-fund to Mr. R. Etheridge, xxix ;
Anniversary Address, February 17,
1871, xxx. Obituary Notices of De-
ceased Fellows:—Mr. Robert Hut-
ton, xxxi; Sir Proby T. Cautley,
xxxi; Lord Chief Baron Sir Fre-
derick Pollock, xxxiii; Dr. Collier,
xxxili; Mr. Bradford, xxxiii; the
Rey. C. Erle, xxxiii; Prof. Gustav
Bischoff, xxxiii. Notices of Papers
published by the Society in 1870 :—
On Glacial and Tertiary geology,
xxxv; on Secondary formations,
xXxxvi; on Paleozoic and metamor-
phic rocks, xxxviii; paleontology,
xxxvlll; colonial and foreign geo-
logy, xxxix; foreign paleontology,
xl; the Palzontographical Society,
xli; address on deep-sea life and its
relations to geology, xlii.
Protospongia? major, 401.
Punfield Cove, section in, 212.
Punfield formation, Mr. J. W. Judd
on the, 207 ; relations of the, to the
Wealden, Neocomian, and Creta-
ceous of the south of England, 221;
foreign equivalents of the, 223.
Purbeck, Isle of, Punfield formation
in the, 211.
Purbeck, relation of the, to the Weal-
den, 222.
Quartz-rock of Banffshire, 102, 104.
Queenstown, section through, 587.
Quitaro river, section from the Ro-
_ Yaima mountain to the, 421.
INDEX TO THE PROCEEDINGS.
Ramsay, Prof. A. C., on the physical
relations of the New Red Marl,
’ Rheetic beds, and Lower Lias, 189.
, on the red rocks of England of
older date than the Trias, 241.
Homusholt, section in the Red Crag at,
Rateau, glacier of the, 318.
Red Clay in the Cape Colony, 520.
Rod rocks of England of older date
pen the Trias, Prof. Ramsay on the,
Reit-poort, ice-scratches at, 541.
Report. Annual, i; of the Library
and Museum Committee, ii.
Reptilian fossils from Gozo, Mr. J.
W. Hulke on some, 29.
Reptilian skull, Mr. J. W. Hulke ona
large, from Brooke, Isle of Wight,
probably Dinosaurian, and referable
to the genus Jguanodon, 199.
Rhetic beds New Red Marl, and
Lower Lias, Prof. A. C. Ramsay
a the physical relations of the,
o
Rhachiopteris, sp., 273.
Rhachiosoma bispinosa, 91.
- echinata, 92.
Rhodanien, 223.
Roches moutonnées of the Katberg,
539.
Rocke’s Bluff, section at, 498; section
through, 515.
Roraima mountain, section from, to
the Quitaro river, 421.
Rooy-Kop, section from, to Port Natal,
59
Rothstock, cirques of the, 314.
Runton Gap, fossils from, 467 ; section
of the Westleton beds on the side of,
468.
Rupununi river, section across, 421.
Sacaonta river, section across, 421.
St. David’s promontory, South Wales,
Messrs. Harkness and Hicks on the
ancient rocks of, and their fossil
contents, 384.
St. David’s valley,
308.
Saliferous beds of the Uitenhage for-
mation, 505; résumé of the, 510.
Saltpan, Government, 505; section
through, 515.
Salt vlei, near Port Elizabeth, 507;
section through, 508.
Sandown Bay, Punfield formation in,
PASE
Sandstone, Table-mountain, 56.
Sawkins, James G., Hsq., geological
section across,
observations
419.
Schaap-Kraal Hoeck, section of, 541.
Scott, Robert H., Esq., on the minerals
of Strontian, Argyllshire, 372.
Scir of Higg, section through the,
287; pitchstone and porphyry cou-
lées of the, 303; section at the base
of the, 305; section at the cliff of
Bideann Boidheach, north-west end
of the, 308.
Seaford, Mr. W. Whitaker on the
chalk of the cliffs from, to Hast-
bourne, Sussex (title only), 92.
Sections of the gravel-brows of the
Thames and Hampshire areas, 25,
26; through the Krantzkop moun-
tain, 57; from the Bluff, Port Natal,
to the Mont aux Sources, in the
Draakensberg, 58; exposed by the
Umgeni river, north of Durban, 59 ;
between the Bluff, Port Natal, and
the Rooy-Kop, 59 ; at the Izinhluza-
balungu caves, 61; through line of
- excavations at Portsmouth, 75; of
beds with Panopee in position, 79 ;
at Whitecliff Bay compared with
borings at Portsmouth, 80; ideal,
showing the relative positions of the
gravel and mud-deposits at Ports-
mouth, 83; of chalk with flints, east
side of Durdle Cove, 95; of cliff
west of Beer Head, 98; of part of
the top of the cliff west of Brans-
combe mouth, 99; from the Spey to
the Deveron, 102; of old pit on Mr.
Colchester’s farm, Sutton, 117; in
old quarry, Sutton, 119; in a pit
5 furlongs H.N.E. from Sudbourne
church, 120; general, of Coralline
Crag, 121; of pit on Broom Hill,
near Keeper’s Lodge, 1 mile W. from
Orford church, 122; in Punfield
cove, 212; of the Punfield formation
in Swanage Bay and the Isle of
Wight, 213; in Worborrow Bay,
216; of the cliff a quarter of a mile
west of Newhaven harbour, 266; in
parts of the western ditch of New-
hayen fort, 266; of the geological
structure of the island of Higg, 287 ;
of interbedded volcanic rocks, on the
east side of the island of Higg, 291;
of interbedded and intrusivevolcanic
rocks on the east coast of Higg, 297 ;
of basalt veins with tachylite edges,
east side of Beinn Tighe, Higg, 299 ;
of basalt veins traversing inter-
bedded dolerites, Kildonan, Figg.
300; of a vein of pitchstone tra-
on British Guiana,
INDEX TO THE PROCEEDINGS,
yersing dolerite, Rudh an Tangairt,
300; of pitchstone filling a cavity in
dolerite, Higg, 301; at the base of
the Scur of Higg, 305; at the cliff
of Bideann Boidheach, north-west
end of the Scur of Higg, 308 ; im the
Red Crag at Ramsholt, 327; in
Bawdsey cliff, 327, 334; in the cliff
at Walton, 328; in a pit on the
common about half a mile west of
Butley Abbey, 329; of the upper
25 feet of the cliff, Walton-on-the-
Naze, 333; in railway-cutting south
of Woodbridge, 334; half a mile
_ west of Shottisham Hall, 335 ; in pit
by side of road 14 mile N.N.K. from
Sudbourne church, 335; in ballast-
pit, Aldborough, 335; at Chillesford,
336; in Chillesford brick-pit, 337 ;
from the railway to the high-road,
near Warren House, 339; in Bul-
lock-yard pit, Sutton, 340; of pit
near the Barn, 340; of pit at Park
Farm, Tattingstone, near Ipswich,
342; of pit near Bulchamp Union,
344; of cliff at Haston Bayent, 345 ;
across St. David’s promontory, 388 ;
from the Roraima mountain to the
Quitaro river, 421 ; in pit at Aldeby,
454; in Thorpe pit, Norwich, 456 ;
in chalk-pit, Coltishall, 459 ; of the
lower part of the cliff west of Sher-
ringham, 460; of the north end of
Southwold cliff, 462; near the north
end of Haston-Bayent cliff, 462; of
the cliff between Kessingland and
Pakefield, 463; of the lower part of
the cliff 14 mile south of Pakefield,
463; of the cliff near Bacton, 464;
in Paston cliff, 465; of the Westle-
ton beds near Mundesley, 467; of
the Westleton beds on the side of
Runton Gap, 468; at Bishopford
bridge, Norwich, 469; collated, on
the Zwartkops river, 498; of the
salt vlei and flat on the south side
of the creek or Ferreira’s river, 508 ;
of outlier near the salt vlei, 509;
showing the relative positions of the
Trigonia-beds, the saliferous group,
anc the Posttertiary shell-limestone
of South Africa, 515; at Dordrecht,
on the Upper Stormberg, 524; on
the Upper Zwart Kei, between the
Great Winterberg and the Groot
Tafelberg, 526; of the Stormberg,
at the source of Klaas-Smit’s river,
531; from the sea at Alexandria to
the Orange river, 537; showing
‘the dip of the Upper Karoo-beds
from Beaufort to the Washbank,
537.
Sedimentary strata of Banffshire &e.,
derivation of the, 106.
Sheets, intrusive, in the island of Higg,
295; section of, 297. :
Shell-beds, latest, in the Cape Colony,
520.
Sherringham, section in cliff near,
460.
Shottisham hall, section near, 335.
Sigillaria, Calamites, and Calamoden-
dron, Dr. J. W. Dawson on the
slructure and aftinities of, 147.
Sigillaria, structure of, 147; erect
trunks of, 148; prostrate trunks of,.
149.
Sizewell cliff, fossils from, 343,
Slates of Banffshire, 104.
Solarium Wiebeli, 65.
Solenastraa Prestwichi, 369.
South-African geology, Mr. G. W.
Stow on, 28, 52, 497, 523.
Southwold cliff, section of north end
of, 462.
Spain, Eastern, coal-bearing strata of,
224.
Spey, section from the, to the Deyeron,
102.
Sternbergie, structure of, 150.
Stoke Edith, Herefordshire, Mr, H.
Woodward on a new species of Hu-
rypterus from Perton near, 261.
Stormberg, coal from the, 51; denu-
dation north of the, 548; section on
the south side of the, at the source
of Klaas-Smit’s river, 531; sections
through, 537.
, Upper, section at Dordrecht on
the, 524.
Stow, George William, Esq., on some
points in South-African geology,-
Part I., 28, 497.
. Parts II. and IIT., 52, 523,
534,
Strontian, Argyllshire, Mr. R. H. Scott
on the minerals of, 372.
Strontianite, 373.
Sudbourne church, pit 5 furlongs HE.
N.E. from, 120; pit 14 mile N.N.E.
from, 335; fossils from, 332.
Suffolk and Norfolk, Mr. J. Prestwich
on the Crag-beds of, with some ob-
servations on their fossil remains.
Part I. The Coralline Crag of Suf-
folk, 115.
. Part II. The Red Crag of
Hssex and Suffolk, 325.
Part III. The Norwich
Crag and Westleton beds, 452,
INDEX TO THE PROCEEDINGS.
Sundays river, section through, 515,
Sutton, section of crag-pit on Mr. Col-
chester’s farm, 117; fossils from
Coralline Crag at, 117, 118, 119;
sections of Red Crag at, 340. |
Swanage Bay, section of the Pun'field
formation in, 213.
Table-mountain sandstone, 56.
Tafelberg, Groot, section on the Upper
Zwart Kei between the, and the
epee Winterberg, 526; sketch of,
47.
Tafelbergen, Twee, sketch of, 5477.
Talcose slate formation of, Natal, 55.
Tate, Ralph, Hsq., on the age of the
Nubian Sandstone, 404.
Tattingstone, near Ipswich, section of
Crag at, 342.
Teleosaurus megarhinus, 442,
Teleosaurian snout, Mr. J. W. Hulke
on a fragment of a, from Kimme-
ridge Bay, Dorset, 442.
Tertiary beds, Mr. W. Whitaker on the
cliff sections of the, west of Dieppe
in Normandy, and at Newhaven in
Sussex, 263.
—— climates of South Africa, Mr.
G. W. Stow on the, 534.
deposits recently exposed at
Portsmouth, Mr. C. J. A. Meyer on
Lower, 74.
or Posttertiary strata of South
Africa, 515.
volcanic rocks of the British
Islands, Prof. Geikie on the, 279.
Teudopsis Brodiei, 448.
Theca antiqua, 400.
Thorpe pit, Norwich, section in, 456 ;
fossils from, 456.
Torcal, 110.
Tree-ferns and other fossils from the
Devonian, Dr. J. W. Dawson on
some, 269.
Trevelyan, Sir W. C., Bart., on sup-
posed borings of Lithodomous Mol-
lusca, 231.
Trigonia-beds of the Uitenhage for-
mation, 498.
Trigonia Shepstone, 66.
Tutts of the island of Higg, 293.
Tullich, hill of, section through, 102.
Uitenhage formation, Trigonia-beds of
the, 498 ; saliferous beds of the, 505.
Umgeni river, section exposed by the,
59
Umtamfuna river, Cretaceous fossils
from, 67.
Unamara river, section across, 421, .
Unconformity between the Cretaceous
and Neocomian in ‘the South of
England, 221,
Urgonien, 223.
Vaal valley, crystalline rocks from, 50.
Valleys, Alpine, Rey. T. G. Bonney
on theories of the excavation of,
812; basin-like, 540. |
Veins in the island of EHigg, 298 ; basalt,
with tachylite edges, east side of
Beinn Tighe, Hige, 299; anamesite
and dolerite, in the island of Higg,
299; pitchstone and felstone in
Higg, 299; basalt, traversing inter-
bedded dolerites, Kildonan, Higg,
300 ; pitchstone, traversing dolerite,
Rudh an Tangairt, Higg, 300.
Volcanic action, Mr. J. J. Murphy on
the connexion of, with changes of
level (Abstract), 108.
Volcanic rocks, Tertiary, of the Bri-
tish Islands, Prof. Geikie on the,
279.
Waetipu mountain, section through,
)
Waldringfield, Prof. Duncan on a new
species of Coral from the Red Crag
of, 369.
Walton-on-the-Naze, sections in the
cliff at, 328, 333.
Warren house, section near, 339.
Washbank, section through the, 537.
Watersheds of Natal, 54.
Wealden and Neocomian, thinning
out of the, in the south of England,
222.
, Neocomian, and Cretaceous of
the south of England, relations of
the Punfield formation to the, 221.
——, relations of the Purbeck to the,
222.
Weald, sections of Punfield beds in
the, 220.
, 8. V. Wood, Jun., Esq., on the
evidence afforded by the detrital
beds without and within the north-
eastern part of the valley of the, as
to the mode and date of the denu-
dation of that valley. 3.
Westleton beds, Mr. J. Prestwich on
the, 461.
Weybourne, Crag fossils from near,
460.
Whitaker, W., Esq., on the chalk of
the cliffs from Seaford to East-
bourne, Sussex (title only), 92.
——, on the chalk of the southern
part of Dorset and Devon, 93.
INDEX TO THE PROCEEDINGS.
Whitaker, W. Hsq., on the cliff-sec-
tions of the Tertiary Beds west of
Dieppe in Normandy, and at New-
haven in Sussex, 263.
Whitecliff Bay, section at, 80.
Whittlesea, section through, 537.
Winterberg, Great, section on the
Upper Zwart Kei between the, and
the Groot Tafelberg, 526.
Wollaston Donation Fund, award of
the Balance of the Proceeds of the,
xxix; Medal, award of the, xxvii.
Wood, 8.V., Jun., Hsq., on the evi-
dence afforded by the detrital beds
without and within the north-eastern
part of the valiey of the Weald as
to the mode and date of the denu-
dation of that valley, 3.
Woodbridge, section in railway-cut-
ting south of, 334.
Woodward, Henry, Hsq., on a new
species of Hurypterus (H. Birodiet)
from Perton, near Stoke Edith,
Herefordshire, 261.
Woodward, H. Esq., on some new
crustaceans from the Lower Hocene
of Portsmouth, 90.
Woolhope, Herefordshire, Rev. P. B.
Brodie on the “ passage-beds” in
the neighbourhood of, and on the
discovery of a new species of Hu-
rypterus and some new land-plants
in them, 256.
Worborrow Bay, section in, 216.
Yarn Hill, fossils from, 346.
Zwart Kei, Upper, section on the, 526 ;
contour-plan of exposures of strata
on the, 527.
Zwartkops river, collated sections on
the, 498.
, section from, to McLough-
lin’s Bluff, 515.
THE END.
Printed by TAYLOR AND FRANCIS, Red Lion Court, Fleet Street,
QUARTERLY JOURNAL
OF THE
GEOLOGICAL SOCIETY OF LONDON,
EDITED BY
THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.
VOLUME THE TWENTY-SEVENTH.
1871.
PARTIT. MISCELLANEOUS.
‘
ey
ae
iy
‘s i
Sa) Gale
CONTENTS OF PART II.
Alphabetically arranged—the Names of the Authors in capital letters.
P
Brachiopoda, Living and Tertiary, of the Kingdom of Naples, Prof. ie
3
G. SEGUENZA on the Nomenclature of the ...........-.2cseee:
Brown Coal of Sagor, Carniola, Prof. C. von ETTINGsHAUSEN on
CME OAV OR EMCO, eerrieiiyd these antics esnlu ba wnn Miey oie mae tee aah at lads
ErTiInasHAUsEN, Prof.C. von. On the Flora of the Brown Coal of
BSH yO AITO eae stare eh 9 Mapah cent Atoee eilakelalie el uni silei eh dasavey ios pie ol a art
Jurassic Series, Dr. M. NeumAYR on Phylloceras in the ..........
Naples, Living and Tertiary Brachiopoda of the Kingdom of, Prof.
. SEGUENZA on the Nomenclature of the .................05:
Neumayr, Dr. M. On Phylloceras in the Jurassic Series ........
Phylloceras in the Jurassic Series, Dr. M. NEUMAyR on ..........
Sagor, Carniola, Prof. C. von ErTINGSHAUSEN on the Flora of the
Ow Olas ynogome sao cenoer con nO bp Udo Oe Rb Noe Ao OorMiond
Sr@ueEnza, Prof.G. On the Nomenclature of the Living and Tertiary
Brachiopoda of the Kingdom of Naples ..........020eeeseeeee
4
1
TRANSLATIONS AND NOTICES
OF
GEOLOGICAL MEMOIRS.
1. Payitoceras in the Jurassic Serres. By Dr. M. Neumayer.
[Imperial Geological Institute, Vienna, June 30, 1871.]
Tt abundance of species of this genus is a paleontological cha-
racteristic of the Mediterranean Jurassic rocks, their occurrence
being comparatively rare in those of the neighbouring middle Ku-
ropean region. In any well-known deposit containing these Cepha-
lopods, four chief types of Phylloceras may be distineuished ; the
representatives brought together from all horizons constitute four
great series of forms, besides which a few isolated species occur.
The members of each series, nearest in geological age, present -
a striking mutual affinity, although the differences between them,
accumulating in the same direction, produce a considerable dis-
crepancy between the oldest and the youngest forms. In the first
place, the sutwral line is continuously modified in one direction,
the division and complication of the sellar leaves gradually in-
creasing. Analogous, but less important, modifications take place
also in the sculpture of the shell; but very little regularity is notice-
able in the modifications of the general form, transverse section, de.
The four series of forms distinguished by the author are as fol-
lows :—
1. Series of Phylloceras heterophyllum.—Sculpture of shell only
simple radial striz or folds; saddles slender, nearly symmetrical ;
termination of the first lateral saddle of the inner side one-leafed.
The species of this series are :—
Phylloceras heterophyllum, Sow. Upper Lias.
trifoliatum, sp. n., Inferior Dogger.
— Kudernatschi, Hauer. Klaus beds.
— Kunthi, sp. n. Kelloway group.
—— plicatum, sp. n. Oxford group.
isotypum, Ben. Aspidoceras-acanthicum beds.
saxonicum, sp.n. Ibid.
serum, Opp. Tithonian.
—— ptychostoma, Ben. Ibid.
—— Thetis, D’ Orb. Neocomian.
_ Pyellede, Mich. Gault.
2. Series of Phylloceras Capitanei.—Internal cast with simple
furrows inclined forward, corresponding to prominences (never to
furrows) of the shell; distinct radial strie, bending forwards ;
saddles slender, unsymmetrical ; first lateral lobe of the inner side
with a two-leaved termination. Species :—
VOL. XXVIJ.—PART II. B
2 GEOLOGICAL MEMOIRS.
Phylloceras Capitanei, Catullo. Middle Lias.
—— Nilsoni, Héb. Upper Lias.
—— connectens, Zitt. Inferior Dogger.
—— heterophylloides, Opp. Middle Dogger.
disputabile, Zé¢t. Upper Dogger and Kelloway group.
—— Demidoffi, Rouss. Of uncertain age (Crimea).
—— Manfredi, Opp. Oxford group.
—— Puschi, Opp. Oxford group.
—— benacense, Cat. Aspidoceras-acanthicum beds.
—— Kochi, Opp. Tithonian.
3. Series of Phylloceras ultramontanwm. — Kneed radial fur-
rows; strie of shell entirely wanting, or only next to the outer
side, and then coarse and short ; lobes and saddles clumsy ; first la-
teral saddle of the inner side with two-leaved termination. Species :—
Phylloceras ultramontanum, Zitz. Inferior Dogger.
—— Zignodianum, D’Orb. Middle Dogger.
—— mediterraneum, sp.n. Klaus beds and Inferior Tithonian.
—— polyoleum, Ben. <Aspidoceras-acanthicum beds.
—— silesiacum, Opp. Tithonian.
—— Calypso, D’ Orb. (=?P. berriasense, D’Orb.). Neocomian.
4. Series of Phylloceras tatricum.—Rounded prominence on the
external side; radial striation very faint, or entirely deficient;
saddles clumsy, first lateral saddle on the internal side (?). Species :—
Phylloceras tatricum, Pusch. Inferior Dogger.
—— flabellatum, sp. n. Klaus beds.
—— Hommairei, D’Orb. Age uncertain (Crimea).
-—— euphyllum, Newm. Kelloway and Oxford groups.
—— ptychoicum, Quenst. Tithonian.
—— semisulcatum, D’Orb. Neocomian.
5. Isolated types.
Phylloceras subobtusum, Kud. Klaus beds.
viator, D’ Orb, Oxford group ?
—— Beneckei, Zit¢t. Tithonian.
—— haloricum, Hauer. Klaus beds.
tortisuleatum, D’Orb. Klaus beds and Tithonian.
The first three of these isolated forms, together with P. Rouya-
num, D’Orb., from the Neocomian, may perhaps constitute a di-
stinct series.
Hach mutation within a series of forms presents very slight but
constant differences, without any gradual transitions. The whole
of the forms of a series may be considered either to belong to a
single species, or to be specifically distinct. The last course seems to
be best adapted for geological purposes; and the genetic connexion
may be indicated by adding to the name of the altered form that of
the form from which it has been derived, under the algebraic symbol
7, aS proposed by Waagen.
The objections against these distinctions as representing vari-
ties rather than genuine species, may be of weight as regards
existing forms, or extinct forms within a given horizon, considered
independently of any succeeding or preceding formation ; but in the
whole chain of successive organisms the species extends into a series
SEGUENZA——NEAPOLITAN BRACHIOPODA. 3
of forms, each representing a distinct phase in the gradual deve-
lopment of a fundamental form.
Wherever the internal lobes could be laid bare, the antisiphonal-
lobe was found to terminate in two points, and the termination of
the adjacent internal saddle to be one-leafed. The termination of
the first lateral saddle is said, by Quenstedt, to be one-leafed in
P. tortisulcatum. The embryonal whorls are nearly alike in all the
spec’es examined, presenting a close external resemblance, on a
very diminutive scale, to certain Goniatites, such as Groniatites
tridens, Sandb. The lobes of examples about 2 millims. in dia-
meter assume a Ceratitic character. [Coonr M.] -
2. On the NomenctatureE of the Livine and Tertiary Bracuropopa
of the Kinevom of Narrzs. By G. Sreuvenza.
[Bollettino Malacol. Ital., 1870.]
Professor Seguenza has published a critical revision of the Brachi-
opoda described by Professor Costa in his ‘Fauna del regno di
Napoli.’ It is founded on the materials collected by Costa, and
leads the author to the following results :—
Costa’s NAMES. CoRRECTED NAMES.
A. Living species.
3 Terebratula vitrea, Born.
I. Derebratula vitrea .......s.....-00+: eh
2. —— caput-serpentis.................. Terebratulina caput-serpentis, Lin.
3. (WANDOYCHNED 7 Hecnoeodo mic nneeaaneecde Megerlia truncata, Lin.
4. Orthis detruncata .................. Argiope decollata, Chemn.
5. HOS icankdacdcnneocappatocadenancse curvata, Risso.
6. —— neapolitana .................668. —— neapolitana, Scacchi.
‘Uo, === LOI bipapptaceniaecnenceencoeeousoone neapolitana ?
So ————— WOMOTAL si.0kestedesesccateness Megerlia monstruosa, Scacchi, jun.
OP MONSHTUOSA, ....2c0cccscecece sss —— monstruosa, Se.
10. Platydia anomioides ................+- Platydia anomioides, Scacchi.
11. Thecidea mediterranea............... Thecidea mediterranea, Risso.
12. Crania personata ...............000... Crania turbinata, Polz.
B. Tertiary species.
1. Terebratula vitrea..................00+ ‘
2. —— caput-serpentis.................. Vide supra.
3. (RUUNEAUID, | cooansdosticdegsondsoaoes :
4. Terebratula grandis .................. He aa: ee
5. buplicatiay ysis benneetwceetsh . ——sinuosa, Brocchi.
(( sinuosa, Brocchi.
minor, Phil.
6. rhage/ GU Vell: prenwenonddsdcossooncne 4 Waldheimia cranium, Mil.
| Tere septigera, Lovén.
Terebratella septigera, Phil.
7 amygdaloides ...............-.- Waldheimia cranium, Mil.
8. Gubliymarssieeeeeea sees sees ear —— cranium, Mill.
To errno es sncacsesocboncesescoune Megerlia eusticta, Phil.
10. —— bipartita ..................00- Rhynchonella bipartita, Brocchz.
11. —— plicato.dentata.................. bipartita, Brocchi.
12. Pauperaiial-eeescse-ee reese der —— pauperata, Costa.
Sel Oxihish li citerameeesneese ssa Argiope decollata, Chemn.
ide detruncatamienceeeeeee eee cane
: Vide supra.
15. Crania personata ..................... P
[Count M.]
4 GEOLOGICAL MEMOIRS.
3. On the Fiona of the Brown Coat of Sacor, CaRnrona.
By Proressor C. von ErrinasHavsen.
[Imperial Academy of Sciences, Vienna, April 13, 1871.]
Ur to the year 1820 only 9 species belonging to this flora were
known, and these were described by Unger in his ‘ Genera et
Species Plantarum fossilium.’ In 1850 Prof. C. von Ettingshausen
commenced a careful investigation of this Flora, representatives of
which are now known to occur in fourteen distinct localities at
Sagor and in the neighbouring districts of Carniola and Styria; and he
has now completed the first part of his description, embracing the
Thallophytes, Vascular Cryptogams, Gymnosperms, Monocotyledons
and Apetala. A species of Spheria from Sagor is most nearly
allied to Spheria annulata from Greenland. A Floridean Alga,
analogous to Lawrencia, indicates the presence of salt water, and is
the only marine plant of the flora of Sagor.
The Gymnosperms number 15 species; and among them is an
Actinostrobus of Australian type, the six-valved strobiles of which has
been found in two localities. The prevalent conifers are Glypto-
strobus europeus and Sequoia Couttsiw, the branches, strobiles, and
inflorescence of which have been met with at nearly every locality.
Other species of Sequoia are S. Langsdorfi, S. Tournali, and S. Stern-
bergi. A new and remarkable fact is the presence of a Cunning-
hamia in these Tertiary deposits. A fragment of a branch strikingly
similar in every respect to Cunninghamia sinensis, R. Brown, has
been found in a quarry near Sayine. The genus Pinus includes
Six species, each generally represented by complete clusters of
leaves and by the cones.
As at Sotzka and Haring, the number of Graminez is very small.
The Najadez are remarkable in numbers and forms, including two
species of Potamogeton, one of Zostera, one of Najadopsis, and one of
Najadonium, all inhabitants of fresh water. The Pandanez and
Palms are each represented by one species. Casuarina sotzkensis,
which is frequent in all Tongrian and Aquitanian floras, occurs —
here, and with it a new species, nearly allied to the existing C.
quadrivalvis. The other apetalous families of the Sagor flora are
represented as follows:—Myricacee by 3, Betulaceree by 6, Cupu-
liferee by 15, Ulmacez by 4, Celtideee by 2, Artocarpex by 2, Sali-
cine by 2, Nyctaginee by 1, Monimiacez by 1, Santalacee by 4,
Daphnoide by 2, Proteacesw by 21, Laurines by 18, and Morezx by
19 species. Most of the species of the last two families present a
tropical aspect. [Counr M. }
TOPOGRAPHICAL INDEX
THE FELLOWS
GF THE
GEOLOGICAL SOCIETY OF LONDON,
Resident in the Country or Abroad.
3G
TOWNSHEND M. HALL, Esea., F.G.S.
[CORRECTED TO JANUARY Isr, 1872.]
NOTE.
Tue following Index is intended to form a Supplement to the ordinary
Alphabetical List, by means of which the name of every Fellow re-
siding in any part of the world may be ascertained at a glance.
To facilitate reference, the aim has been to group, in each county,
the various localities around their respective post-towns. Names of
streets and houses have been omitted; but those of parishes and more
distant estates have been inserted whenever it appeared requisite.
The only inconvenience attending the adoption of this rule will be
found in the very few instances where the residence of a Fellow is
situated in one county and his post-town in another.
Much of the difficulty experienced in the preparation of the Index
has arisen from the incomplete and inaccurate descriptions frequently
given. The attention of Fellows is therefore again directed to the
request of the Council, that all changes of residence should be imme-
diately communicated to the Secretary, who will also gladly receive
corrections of any errors.
TOWNSHEND M. HALL.
Pilton, Barnstaple,
Jan. Ist, 1872.
I. RESIDENTS IN GREAT BRITAIN AND IRELAND,
EXCLUSIVE OF THOSE WHO LIVE WITHIN THE LIMITS
OF THE LONDON POSTAL DISTRICT.
ENGLAND.
BEDFORDSHIRE.
Bedford—Sanders, Rey. 8. J. T. | Bedford—Wyatt, J.
BERKSHIRE.
Ascot—Everest, Rev. R. Wallingford (Aston Tirrold)—Rome,
Maidenhead (Taplow) —- Serocold, Rey. J. L.
CrP. Wantage—Davey, E. C.
Newbury—Valpy, R. H. Windsor (Clewer)—Harris, W. H.
Sandhurst—Fothergill, Capt. C. W. | Wokingham—Bentinck, Gen. A. C.
BUCKINGHAMSHIRE.
Aylesbury—Hunt, Z. D. Great Marlow—W oodman, W.
(Aston Abbots) — Thornton, | High Wycombe—Browne, Rey. T. H.
Rev. J. Newport Pagnell—Bull, Rev. J.
CAMBRIDGESHIRE,
Cambridge—Babington, Prof. C. C. Cambridge—Routh, E. J.
Bonney, Rey. T. G. Sedewick, Rey. Prof. A.
—— Cartmell, Rev. J. — Seeley, H.
—— Danby, T. W. — Worsley, Rey. T.
—— Miller, Prof. W. H. —— (Harlton)—Fisher, Rey. O.
—— Phear, Rey. S. G.
CHESHIRE.
Alderley Edge—W aters, A. W. Rock Ferry—Roberts, I.
Altrincham—Brooke, W. Stockport—Barr, W. R.
Birkenhead—Bretherton, E. (Poynton)—Greenwell, G. C.
—— Ferguson, W. Tarporley—Keerton, Sir P. de M. G.
—— Ricketts, C. Wallasey—Hall, HW. F.
CoRNWALL.
Falmouth—Collins, J. H. Redruth—Davey, R.
Helston—Vyvyan, Sir R. R. Richards, T.
Pelynt—Kendall, N. Scilly Isles—Smith, A.
Penryn (Enys)—Enys, J. 8. Truro (Goonvrea) — Williams, Sir
Penzance—Courtney, J. 5. F, M.
Henwood, W. J. — (Polwhele}—Polwhele, T. R.
— Higgs, S.
b
6
CUMBERLAND.
Alston—Paull, J. M. Keswick—Ward, J. C.
Carlisle (Brigham Hill)—Fletcher, | Penrith—Nicholson, H. A.
W. (Ulleswater)—White, Rev. F.
— (Haydon Bridge)—Bewick,T.J. Le G@
( Tarnbank)—Fletcher, If, Whitehaven—Dees, He
Cockermouth (Wood Hall)—Fisher, | —— Dixon, G.
J.C. —— Moon, M. A.
DERBYSHIRE.
Ashbourne (Ilam)—Russell, J. W. Derby—Fearn, 8. W.
Belper—Evans, T. (Milford )—Strutt, Hon. A.
Chester field (Brampton)—Mello, Rey. |
5 Hs
J
DEVONSHIRE,
Barnstaple—Hall, Townshend M. North Lew—England, Rev. T.
Harding, Lt.-Col. W. _| Plymouth—Jackson, E. S$
Hore, Rey. W. 8. Stonehouse—Coles, J.
Buckfastleigh—Gale, J. Teignmouth—Cooke, H.
Exeter—Jerwood, J. Ormerod, G. W.
Lingwood, R. M. Torquay—Hunt, A. R.
—— Templeton, J. Lee, J. E.
— Vicary, W. — Pengelly, W.
—— (Kenton)—Pycroft, G. Tawney, E. B.
(Lympstone)—-HKdgell, A. W. Totness—Champernowne, A.
Honiton (Holyshute)—Swann, Capt.
dis Si
DOoRSETSHIRE.
Blanford (Whatcombe) — Mansel- | Sherborne (Holwell)—Wood, Rey.
Pleydell, J. C. Teh, Jel
Charmouth—Breton, Capt. W. H. Weymouth—Damon, R.
Dorchester (Stafford) —Floyer, J. Drew, J.
Langton Maltravers—Lester, L. Wimborne—Austen, Rey. J. H.
Sherborne (Bradford Abbas)—Buck-
man, J.
DuRHAM.
Blaydon-on- Tyne—Simpson, J. B. Durham—Farrar, Rev. A. S.
Darlington—V’ Anson, J. C. Ferry Hill (Wingate Grange)—Arm-
Koma, R. strong, W.
—— Spark, H. K. Gateshead—Favell, T. M.
— Tait, R. ( Usworth)—Coxon, 8. B.
—— (Raby Castle)—Scarth, W. T. South Shields—Lyall, G.
EssEx.
Brentwood—W ood, 8. V. Colchester (Thorpe)—Watson, J. Y.
Wood, 8S. V., Jun. Harlow (Sheering)—Hill, Rev. E.
Buckhurst Hill—Babington, W. Maldon ( Ulting)—Piggot, J.
Chelmsford—Church, J. Saffron Walden (Audley End)—Old-
Cer (Stanway)—Jenkyns, Rev. ham, Rev. J. L.
i
é
Essex (continued).
Saffron Walden (Chesterford)—
Hervey, Rev. Lord C. A.
—— (Wimbish)—Montague, Rev. J.
Shoeburyness—Innes, Lieut. W.
Stratford—Brady, Sir A.
Wanstead—W alker, F.
GLOUCESTERSHIRE.
Bristol—Cossham, H.
—— Pease, T.
— Stoddart, W. W.
—— (Bitton)—Parker, J.
—— (Chfton)—Brough, L.
— King, W. P.
—— —— Sanders, W.
Sisson, W.
—— (Henbury)—Perceval, 8. G.
(Redland)—Austen, Major T,
Cheltenham—Bevan, G. P
Bloxam, T.
Bright, J.
Copeland, G. F.
Orchard, J. W.
Smithe, Rey. F.
Wright, T.
Cirencester—Bravender, J.
Gloucester —Cadle, C.
(Brookthorpe)—Lucy, W. C.
Gloucester (Elmore Court) — Guise,
Sir W. V.
(Hardwick Court)—Baker, J.
B
aes (Hucclecote)—White, He.C:
—— (Tibberton Court)—Price, Capt.
W. E.
LIydney—Philpot, Rey. B.
Newnham( Bilson House)—Thomas,A.
Stow-on-the- Wold—Witis, Rev. E.F.
Stroud—Paine, W. H.
Witchell, E.
Tewkesbury (Forthampton)—Y orke,
JR
(Kemerton)—Thorp, Archdea-
con.
(Pendock)—Symonds,Rey. W.S.
Wotton-under-Edge (Tortworth)—
Ducie, Earl of.
— (Wickwar)—Preston, L.
HAMPSHIRE.
Aldershot—Home, Capt. R.
Hutchinson, Capt. A. H.
Alton (Selborne)—Bell, T.
Fareham ( Crofton)— Wingate, SirG.
Horndean—Martin, J.
Portsmouth—Martin, J.
Weston, W.
Southampton—James, Sir H.
(Merry Oak)—Fovrbes, J. H.
Stoney Cross—Hyre, G. E.
Winchester—Shelley, G. E.
Winchfield (versley)—Kingsley,
Rey. C.
Isle of Wight.
Freshwater—Pritchard, Rev. C.
Newport— Wilkins, E. P.
HEREFORDSHIRE.
Hereford—Curley, T. |
Ledbury (Hatfield)—Henry, W. C.
HERTFORDSHIRE.
Albans, St.—Kernahan, Rev. J.
(Sandridge)—Winbolt, J. 8.
Cheshunt—Mayo, H.
Hemel Hempstead—Eyans, J.
Hemel Hempstead—Longman, C.
Stevenage (Gravely)—Denton, J. B.
Watford— Humbert, C. F.
Welwyn (Danesbury)—Blake, W. J.
Kent.
Ashford (Charing)—Harris, W.
Bromley—Child, C.
Hamilton, A.
— Lubbock, Sir J. |
— Norman, G. W.
Canterbury—Bell, M.
Collard, T. W.
Deal (Northbourne)—Cooke, Rey. 8.
H
Dover—Knowles, Rev. J.
62
KEnvT (continued).
Folkestone—Lanedon, Rey. E.
Gravesend—Gladdish, W.
Guest, Rev. W.
Ih, ythe—Mackeson, H. B.
Sandwich (Betteshanger )—James, Sir
50
Sevenoaks—Browne, R. G. M.
(Shoreham)—Prestwich, J.
Tunbridge Wells—McClean, F.
Sharp, J.
— Spratt, Capt. T. A. B.
Thornton, Rey. W.
—— (Br oadwater) —Gibson, UR
(Groombridge)—Cooke, Hi. W.
West Malling—Timins, Rey. J. H.
Wingham (Stourmouth)—Dowker, G.
LANCASHIRE.
Blackburne—Kiccles, J.
Lancaster—Diz ens, J.
Rofe, J.
Prosser, W.
Liverpool—Cunningham, J.
Eskrigge, R. A.
Hall, H. F.
Morton, G. H.
Shoolbred, J. N.
|
Manchester—Binney, EK. W.
Brockbank, W.
Darbyshire, R. D.
Dickinson, J.
Dorning, E.
Forbes, J. E.
Greg, R. P.
Lingard, J. R.
Lynde, J. G.
Smith, F.
(Ardwick)—Fairbairn, Sir W.
eee
( Grassendale)— Duckworth, H.
Manchester (Bacup)—Aitken, J.
(Broughton)—Higson, P.
—— Caen Moor)—Bates, Rev.
J.C
—— (Hollinwood )—Booth, I.
— (Norcliffe)—Greg, R. H.
— (Rusholme)—Darbyshire, R. D-
Dawkins, W. B.
—— (Salford)—Plant, J.
Williamson, EH.
Preston ( Samlesbury )—Harrison, W.
Southport—Willacy, Rev. T. R.
Ulverston—Kennedy, M.
- Salmon, W.
(Grange)—Beardsley, A.
W ae eden ( Thelwall) —Rylands,
G
o \Ke
Whalley—N orwood, Rev. 8.
Wigan (Ashfield)—Laneaster, J.
(Haigh)—Hewlett, A.
LEICESTERSHIRE.
Ashby-de-la-Zouch (Overseal)—
Woodhouse, J. T.
Leicester— Drake, F.
Everard, J. B.
— Plant, N.
?
Leicester (Humberstone) —Bosworth
J. A.
Loughborough (Barrow-on-Soar )—
Crossley, J. 8.
Hambly, C. H. B.
LINCOLNSHIRE.
Boston—Shaw, J.
Brigg (Appleby)—Cross, Rev. J. E.
Gamsborough (Highfield)—Burton,
F. M.
Gainsborough (Saundby )—Chamber-
lain, Rev. T. C. B.
Louth '(Elkington)—Whinfield, E.W.
MIDDLESEX.
Enfield—Kitching, A. G.
Harrow—Leat, C. J.
Stanwell—Waugh, H.
Sunbury House—Lendy, Capt. A. F.
Sunbury Park—Arden, R. HE.
Uxbridge (Dawley)—De Salis, W. F.
MonMOUTHSHIRE.
Caerleon—Lee, J. E.
Chepstow (Sedbury)—Ormerod, G.
Newport—Mitchell, F. J.
Newport—Roper, R. 8.
Pont-y-Pool—Llewellyn, D.
Usk—Falconer, T.
NORFOLK.
Downham Market (Denver)—Stokes,
Rev. W. H.
Lynn (Tilney)—Currie, Rey. C.
Norwich— Charlesworth, E.
Fitch, R.
—- Morant, A. W.
— (Blofield) —Turnbull, Rey. T.S.
Norwich (Heigham)—Harmer, F. W.
— (irstead)—Gunn, Rev. J.
Stoke Ferry (Oxburgh)—Thurtell,
Rey. A.
Yarmouth, Great—McClean, W. C.
Rose, C. B.
NorTHAMPTONSHIRE.
Kettering—Heighton, H. J.
Northampton (Dallington)—Sharp,S.
(Overstone Park )—Overstone,
Lord.
Oundle (Elton)—Lawrance, J.
Rothwell—Glass, Rev. N.
NorTHUMBERLAND.
Berwick-on-Tweed—Home, D. M.
Newcastle-on- Tyne—Bainbridge, W.
Barkas, T. P.
Belt, T.
Brady, H. B.
Johnson, J.
Maclennan, Rev. A.
—— (Blackworth)—Foster, G. B.
—_—_
Newcastle-on-Tyne (Bywell)—Beau-
mont, W. B.
(Wallington) —Trevelyan, Sir
W.C
North “Sihetds ( Tynemouth)—Dag-
lish, J.
Riding Mill—Hurst, T. G.
NoTTINGHAMSHIRE.
Newark-upon-Trent—Brookes, J.
Kendall, Rev. W. C.
Nottingham—Dixon, Rey. R.
Lowe, E. J.
—— Tarbotton, M. O.
Nottingham (Newstead Abbey)—
Webb, W. F.
Southwell—Warrand, Major W. E.
Worksop (Shire Oak)—Tylden-
Wright, C.
OXFORDSHIRE.
Banbury—Pidgeon, D.
Oxford—Gayner, C.
Macbride, J. D.
—— Parker, J.
— Phillips, Prof. J.
—— Pritchard, Rev. C.
Oxford—Prout, Rev. T. J.
Wyndham, T. H. G.
Ror ( Wathngton)—Lucas,
Rey. 8.
Witney (Tynsham)—Mason, J.
SHROPSHIRE.
Broseley ee G.
Iudlow—Lighthbody, R
Madeley—Randall, J.
| Welrngion (Donnerville)—Eyton,
Market Drayton (Norton-in-Hales)—
| Whitchurch—Egerton, Rev. W. H.
Silver, Rey. F.
10
SoMERSETSHIRE.
Bath—Blomefield, Rey. L.
Moore, C.
Robbins, G.
Walker, T. F. W.
Weston, C. H.
Winwood, Rey. H. H.
Bridgewater (Fyne Court)—Hamil-
ton, J.
Bristol (Long Ashton)—Rogers, G.
Evercreech—Talbot de Malahide,
Lord.
Gilastonbury—Pope, C.
| Somerton (Kingweston)—Dickinson,
F. H.
Taunton—J ones, W. A.
Wellington (Nynehead)—Sanford,
W. A.
Weston-super-Mare—Browne, Arch-
deacon, R. W.
Mortimer, W. H.
Pooley, C.
Wrington—Daubeny, R. H.
STAFFORDSHIRE.
Bilston—Bowkley, 8.
Burton-upon-Trent—Brown, E.
Knobel, E. B.
Molyneux, W.
Leek—Wardle, T.
Lichfield—Johnson, J. T.
Penkridge (Rodbaston)— Ward, 1.
Stone— Wynne, T
Walsall (Cannock Chase) —Brown, J.
-—~ (Pleck)—Bailey, 8.
West Bromwich—Cooksey, J.
W olverhampton—Beckett, H.
Cope, J.
— Myers, HE.
—— (Donington)—Jones, D.
— (Willinghall)—Parton, T.
SUFFOLK.
Bury St. Edmunds (Barton)—Bun-
bury, Sir C. J. F
Ipswich ( Grundisburgh)—Colchester,
W :
Saxmundham—Cavell, E.
Saxmundham (Hurts Hall)—Long,
W
Sudbury ( Assington)—Gurdon, J.
Woodbridge (Melton)—Ansted, Prof.
ID), 48 i
SURREY.
Carshalton—Tylor, A.
Wallace, J.
Croydon—Crowley, J. 8.
Flower, J. W.
Lee, H.
Dorking (Katlands)—Heath, D. D.
Godalming—Nevyill, W.
Godstone—Noel, E.
Guildford—Capron, J. R.
— Sells, T. J.
— - Warren, Capt. C.
Guildford _ (Chilworth) — Godwin-
Austen, R. A.
Moulsey, East—W hitaker, W. W.
Reigate—Lainson, H.
(Merstham)—Joliffe, Hon. H. H.
(Redhill) —Brass, Rev. H.
Weybridge—Colvin, A.
(Addlestone)—Rigby, J. B.
Tulk, J. A.
Yorktown—Jones, Prof. T. R.
SUSSEX.
Brighton—Davidson, T.
Jackson, A. W.
Laing, 8.
White, J.
Chichester—M ackintosh, D.
(Lavant)—Robinson, A.
Clayton—Briggs, Gen. J.
Cuckfield—Hankey, J. A.
Forest Row—Slack, H. J.
Grinstead, E.( Felbridge)—Gatty,C.H.
Grinstead, E. (Twyford)—Trotter, R.
Hastings (Hollington) — Wollaston,
GPE
Petworth (Bignor)—Hawkins, J. H.
St. Leonard’ s-on-Sea—Beckles, 8. H.
—— Bowerbank, J. 8.
— Parish, Sir W.
Peyton, J. KE. H.
Shoreham (Southwick)—Pullen, M.
11
W ARWICKSHIRE.
Birmingham—Allport, 8.
Lloyd, G
—— Shaw, G.
— (Aston Manor)—Stone, J. B.
—— (Ldgbaston)—Crosskey, Rev.
EI
— — Matthews, W.
Ratcliff, C.
— (Moseley)—Dawes, J. 5.
Deane, Rey. G.
— (Saltley)—Gover, Rev. W.
Birmingham( West Heath)—Dawson,
G.
Coventry (Allesley)—Wyles, T.
(Berkswell) —W atson, Rey. H.
Rugby—Sharp, W.
— Wilson, J. M.
(Bilton)—Lancaster, J.
Tamworth—Spruce, 8.
Warwick—Kirshaw, J. W.
(Rowington)—Brodie, Rev. P. B.
WILTSHIRE.
pecrham ( Castle Combe)—Scrope,
alae
Corsham—Randell, J. 8.
Ramsbury—Burdett, Sir R.
Salisbury—Duke, E.
Hamilton, Dean H. P.
Devizes (Hilwor #i)—Cunnington, W. — (Baverstock)—Hony, Arch-
Pewsey—Dixon, deacon W. EH.
‘WORCESTERSHIRE.
Broadway (Middle Hill)—Phillips,
Sir T.
Bromsgrove (Dale Cross)-—Walton,E.
Dudley (Oakham)—Minton, S.
Evesham (Hampton, Gt.)—Safford,
J. B.
—— (Harvington)—Ingram, Rev. A.
H.W.
Malvern, Great—Grindrod, R. B.
( Cradley) —Jauncey Ww.
Stourbridge—Fletcher, Major At Ww.
Pearce, H.
(Wordsle y )—Pentecost, J.
Worcester—Baxter, T.
Lees, E.
— Bee EL, H. B.
Viouinsimes.
Barnsley—Dawes, G.
Bedale ( Clifton Castle) —Pulleine, J.
Beverley (Brandsburton) — Hymers,
Rey.
Bradford—McLandsborough, J.
Doncaster—Armstrong, Prof. G. F.
Guisborough—Morgan, Rey. F. H.
Hahfax—Gledhill, J.
( Wellhead) —W. aterhouse, J.
Huddersfield (Edgeston)—Brooke, E.
(Rastrick)—Clay, J. T.
Hull (Hessle)—Smith, TI.
Leeds—Filliter, KE.
Lupton, A.
—— Marshall, A.
— Marshall, J. G.
Richardson, J. W. H.
Normanton (Altofts)—White, J. T.
Oswaldkirk (Wass)—Brown, R. E.
Ouseburn—Abbay, Rev. R.
Richmond—Bradley, C. L.
Bradley, L.
— Wood, E.
—--- Yeoman, H. W.
— (Draycott)—Denys, Sir G. W.
Saltburn-by-the-Sea—Jones, J.
Scarborough—Leckenby, J.
Rooke, C.
Woodall, J. W.
Sheffield—Carrington, T
Jeffcock, T. W.
—— Wall, G. P.
—— (Broomfield)—Sorby, H. C.
Stuart,
Silkstone (Bretton)—Beaumont, W. B.
Skipton (Carleton)—Kddy, J. R.
Thirsk (Brekenbrough)—Hinks, T.C.
ork—Allen, E.
Blake, Rev. J. F.
Gray, W.
Moiser, H. R.
Mosley, G.
Noble, T. 8.
North, 8. W.
Reed, W.
Walker, J. F.
(Hayton)—Ayrundell, Rev. T.
—— (Whexley)—Ford, J.
—— (Whitwell)—Harcourt, E. V. V
Pa
WALES.
CAERMARTHENSHIRE.
Caermarthen—Morris, Rey. R. H.
Bishop of.
(Abergwili)—St. David’s, Lord |
Llandeilo (Dolau-cothy)—Johnes, J.
Llanelly (Nant. aaa dail:
CABRNARVONSHIRE,
Beddgelert (Bryn Gwynant)—W yatt, | Portmadoc—Spooner, C. EH.
J.
FLINTSHIRE.
Hawarden—Moftat, T.
Mold (Bryn Alyn) —Cooke, Rey. R.B
| Wrexham ( Cymmau Hall)—Sparrow,
J.
GLAMORGANSHIRE.
Aberdare—Clark, W. 8.
— Kirkhouse, H.
-—— (Mardy)—Lewis, W. T.
Bridgend—Brogden, J.
(Nottag ge)——Jordan, H. K.
Cardiff—Adams, W.
Brown, TF,
(We envoe)—J enner, R. F. L.
Merthyr Tydvil(Dowlais)—Clark,G.T.
Neath—Richardson, J.
( Cadoxton) —Lewis, L. T.
Swansea—Benson, 8.
Beor, E. J.
Mogeridge, M.
Pearce, R
Tremellen, J. H.
—— (Bishwell)—Brown, F. H.
— (Glenrafon)—Richardson, J. C.
ay ey efoilan)—Dillwyn, L. L.
— (Singleton)—Vivian, H. H.
— (Stout Hall)—Wood, Col. E. R.
MERIONETHSHIRE.
Dolgelly—W iliams, W. R.
| Dolgelly (Mallwyd)—Readwin, T. A.
PEMBROKESHIRE.
Haverfordwest ( Williamston)—Scourfield, J. H.
RADNORSHIRE.
Rhayader—Richardson, R.
SCOTLAND.
ABERDEENSHIRE.
Aberdeen—Macdonald, A.
Nicol, Prof. J.
Aberdeen, Old—Dann, R.
Ellon—Jamieson, T. F.
ARGYLESHIRE.
Inverary Castle—Arg ay, Duke of.
Islay—Campbell, J. F
| Toward Point—Lamont, J.
13
BERWICKSHIRE.
Kames—Hood, T. H. C.
CAITHNESS.
Thurso—Miller, J.
EDINBURGHSHIRE.
Edinburgh—Chambers, W. Edinburgh—Page, D.
Etheridge, R., Jun. Thomson, Prof. W.
— Geikie, Prof. A. Trotter, C.
—— Gillespie, W. Leith—Lundy, J. J.
— Jack, R. L. Muir House—Davidson, T.
FIFESHIRE.
Falkland—Gibb, Sir G. D. | St. Andrews—McDonald, Prof. W.
FORFARSHIRE.
Dundee—Boase, H. | Reswallie—Powrie, J.
INVERNESSHIRE.
Inverness—Mitchell, J. | Skye, Isle of—Matheson, Sir J.
KiRKCUDBRIGHTSHIRE.
St. Mary’s Isle—Selkirk, Earl of.
LANARKSHIRE.
Blantyre—Bryce, J. Glasgyow—Thomson, J.
Glasgow—Bryce, J. Young, Prof. J.
Gregory, T. C. Lanark—Lindsay, C.
— Robertson, D. Monkland—Murray, W.
LINLITHGOWSHIRE.
Torbane Hili—Gillespie, W.
PERTHSHIRE.
Duncrub House—Rollo, Lord. Inchture (Rossie Priory)—Kinnaird,
Perth—Sherwill, Lt.-Col. W. 8. Lord.
RENFREWSHIRE.
Johnstone Castle—Houstoun, G. L.
STIRLINGSHIRE.
Bridge of Allan—Miller, J.
14
IRELAND.
ANTRIM.
Belfast—Boyd, N. Belfast (Holywood)—Anderson, J.
Haslett, 8. De a J. J.
— Wright, J. Larne—Holden,
Cork.
Cares (Killeedy)—Petrie, rel Cork—Jennings, F. M.
F. W. (Drifney Castle)—Colthurst, J.
Cor j—Harkness, Prof. R.
DvuBLIN.
Dublin—Baily, W. H. Dublin—Haull, Prof. E.
— Griffith, Sir R. J. (Malahide)—Talbot de Mala-
— Hamilton, C. W. hide, Lord.
— Haughton, Rev. Prof. S.
FERMANAGH.
Enniskillen (Florence Court)—Enniskillen, Earl of.
GALWAY.
Gort (Lough Cultra)—Gough, Viscount.
KILDARE.
Curragh—Parker, Capt. F.G.S.
LIMERICK.
LInmerick—Prevost, Lieut. L. de T.
Mayo.
Balhna—Symes, R. G.
SLIGO.
Shgo (Abbey View)—Wheatley, J. H.
TYRONE.
Strabane—Ogilvy, W.
WATERFORD.
Waterford (Summerville)—Fortescue, Hon. D. F.
15
CHANNEL ISLANDS.
GUERNSEY.
Carey, Sir P. 8. Musson, E. C.
Collings, Rev. W. T.
JERSEY.
Le Feuvre, W. H. | Peacock, R. A.
II. FOREIGN LIST.
AMERICA, UNITED STATES OF.
ALABAMA. New York—Hawkins, B. W.
: —— Kimball, J. P.
Montgomery—Tait, Col. I. L. Sa (Th eres). Lloyd, T. G. B.
CALIFORNIA.
OxIo.
Cinconnati— Vincent, Prof. M. C.
Cleveland—Humiston, Prof. R. F.
San Francisco—Rowlandson, T.
CONNECTICUT.
Newhaven—Dana, Prof. J. D. PHILADELPHIA.
Boren rorsd: ©: Philadelphia—Leidy, J.
Lesley, Prot. J. P.
MASSACHUSETTS.
Boston—Rogers, W. B. VIRGINIA.
Cambridge—A gassiz, Prof. L. Richnend—Manzy, M.
a CIB WISCONSIN.
Albany—Hall, J. é :
Roper Blen d, T. Madtson—Hobbins, J.
Day, E. C. H.
ANGOLA.
Brand, G.
ARGENTINE REPUBLIC.
Buenos Ayres (San Juan)—Rickard, Major F. I.
AUSTRALIA.
ia eset none Biden, W. D. Newcastle—Keene, W.
St. Leonards—Clarke, Rev. W. B.
New SoutH WALEs. Sydney.—Hunt, R.
Cassilis, Hunter River—Busby, A. Josephson, J. F.
16
AUSTRALIA. (continued).
QUEENSLAND. VICTORIA.
Ipswich—Harlin, T. Maldon—Salter, W.
Rockhampton—Plews, H. T. Melbourne—Clarke, J.
M°Coy, Prof. F.
SouTH AUSTRALIA. Sta et nee ML
Adelaide—Ayers, Hon. H. — Ulrich, G. H. F.
Penola—W oods, Rev. J. E. T. —— (St. Francis) —Bleasdale,Rev.J.
AUSTRIA.
Vienna—Boué, A. BouEMIA.
—— Breunner, Count A.
Hauer, F. R. von. Prague—Barrande, J.
—— Marschall, Count A. G.
== Reuss, Prof A. BE, HUNG AEE:
— Suess, Prof. HE. Pesth—Szabo, Prof. J.
Stuhlweissenberg—Schvarcz, J.
BELGIUM.
Brussels—Gomonde, W. H. Ciney (Halloy)—Halloy, J. J. d’O.
— Nyst, P. Inége—Dewalque, Prof. G.
— Van der Maelen, P. Koninck, Prof. L. G. de.
CANADA.
Seen Elwin, H. Montreal—Dawson, J. W.
Darlington (Beaumanville)—Reid, Logan, Sir W. E.
Capt. J. H. — Nicholson, Prof. H. A.
Montreal—Armstrong, Prof. G. F. — Selwyn, A. R.
Bell, Prof. R. —— Vennor, H. G.
— Billings, E. Whiteaves, J. F.
—— Broome, G. Ottawa—Grant, J. A.
— Colquhoun, J.
CAPE OF GOOD HOPE.
Hike dat uses Bolton, Major-Gen. D. Graham’s Town—Atherstone, W. G.
ais etre Hertzog, W. F. Namaqualand (Fontaux) — Davis,
ogo0ne0S Thurburn, Capt. H. J. F.
CEYLON.
ealncieg Caley, J. A. Colombo—Roosmalecoeq, A. H.
erento ts Kelaart, E. F.
DENMARK.
Copenhagen—Steenstrup, Dr
EGYPT.
Ayrton, F.
17
Brongniart, Prof. A. T.
Daubrée, Prof. A.
Delesse, Prof. A.
Verneuil, E. de.
Vibraye, Marquis de.
Watson, J. G. W.
FRANCE.
Marseilles—Coquand, H. Paris—Deshayes, Prof. G. P.
Montpellier—Gervais, P. Desnoyers, J.
Martins, C. — Edwards, Prof. H. M.
Nantes—Clipperton, Capt. R. C. — Ganudry, A.
Paris—Barrande, J. — Hébert, Prof. E.
Basterot, Baron de. —— Quain, J.
Beaumont, E. de. — Raulin, V.
ane
GERMAN EMPIRE.
BavEN. Saxe Wemar EISENACH.
Heidelberg—Bunsen, Prof. R. W. Eisenach—Sentt, F.
BaVaRIA. Saxony.
Munich—Giimbel, C. W. Dresden—Geinitz, Prof. H. B.
Wiirzberg—Sandberger, Prof. F. Freiberg-—Cotta, Prof. B.
Leipsig—Naumann, Prof. C. F.
HANOVER. Zirkel, Prof. F.
Gottingen—W altershausen, Baron
WS Son. WurRTEMBERG.
Stuttgart—Jager, G. F.
Hesse DARMSTADT. Tiibingen—Quenstedt, Prof.
Darmstadi—Kaup, J. J.
SaxE Cospure GoTHaA.
Gotha—Credner, Herr.
GIBRALTAR.
Gibraltar, Lord Bishop of. | Luard, Capt. C. E.
GREENLAND.
Noungme—Taylor, J. W.
HOLLAND.
Maestricht—Bosquet, J.
Se taeeiens Foote, R. B.
Soialecaihs Margesson, Capt. P. D.
Semele. Oldfield, R. C.
ES a ee Osborne, Lt.-Col. W.
seas MPS. c Roberts, W. H.
3 Rei taeee Sowerby, W.
18
INDIA (continued).
BENGAL.
Drummond, Capt. H.
se erome ac Jack, Capt. A.
Allahabad—Carnac, H. R.
Mackesy, Major W. H.
Beerbhoom—Barker, R. A.
Caleutta—Binnie, A. R.
Blanford, Prof. H. F.
Blanford, W. T.
Leonard, H.
McClelland, J.
Mallet, F. R.
Mason, J. W.
Medlicott, H. B.
Oldham, T.
Phear, J. B.
Stoliczka, F.
Dacca—Clarke, C. B.
Deoghm—Calvert, J.
Raneegunge—W hitfield, J.
BomBay.
Bombay—Cooke, T.
Fedden, F.
Bombay—Goodenough, Lt.-Col. W.
H
— Grant, Capt. C-aWwe
— Rogers, A.
CENTRAL PROVINCES.
Nagpore—Cline, G. W.
KASHMERE.
Drew, F.
Manpras.
Madras—Aitchison, Major-Gen. J.
Ouchterlony, Lieut. J.
NortTH-wrst PROVINCES.
Roorkee—Smith, Col. R. B.
PUNJAB.
‘Wynne, A. B.
Lahore—Purdon, W.
Madhapoor—Smithe, J. D.
? Maleoa—Sylvester, J. H.
ITALY.
' Bologna—Capellini, Prof. G.
Florence—Devincenzi, G,
Sloane, F. J.
Milan—Borromeo, Count V.
Padua—Zigno, Baron A. de.
Piedmont (Val ad’ Ossola)—Foster,
C. Le N.
Pisa—Fairman, E. St. J.
Pisa—Meneghini, Prof. G.
Rome—Ponzi, Sig.
| Turin—Gastaldi, B.
Jervis, W. P.
Perazzi, C.
Sella, Q.
Sismonda, Prof. A.
JAPAN.
Nagasaki (Takasima)—Potter, F.A. | Yokohama—Brunton, R. H.
MADEIRA.
Watson, Rev. R. B.
MALTA.
Caruana, A. A.
Lewis, Lieut. J. F.
Williams, Capt. J.
MAURITIUS.
Cooke, Lt.-Col. A. C,
19
MEXICO.
Pike, J. W.
NATAL.
Wathen, G. H.
NEW ZEALAND.
Bay of Islands—Taylor, Rev. R. Wellington—Crawford, J. C.
Christ Church—F raser, Rev. C. Hector, J.
Haast, J. — Hutton, F. W.
Hood, T. H. C. — Lyon, W.
Wanganuwi—Buller, W. Mantell, W. B.D.
NEWFOUNDLAND.
St. John’s—Murray, A.
NORWAY.
Christianta—Kjerulf, T. | Krageree—Dahll, T.
NOVA SCOTIA.
Cape Breton—Poole, H. 8. | Halifax—Honeyman, Rey. D.
PERSIA, NORTH.
Tiflis—Abich, H.
PERU.
Lima—Quiros, F.
PORTUGAL.
Alemtejo (Pomarou)—Mason, J.
PRUSSIA.
Berlin—Beyrich, Prof. E. Bonn—Dechen, H. von.
Ehrenberg, Prof. C. G. Breslau—Goeppert, Prof. H. R.
Rose, G. Roemer, Prof. F.
Bonn—Burkart, J.
RUSSIA.
Dorpat—Keyserling, Count A. von. | St. Petersburg—Helmersen, Gen. G. v.
St. Petersburg—Brandt, J. F. Kokscharow, M. von.
SPAIN.
Gavey, G. E.
20
STRAITS SETTLEMENTS.
Singapore—Logan, J. R.
SWEDEN.
Iund—Nilsson, 8. Stockholm—-Lovén, 8.
Torell, Prof. O. Nordenskiéld, Prof. A. E.
Orebro—Smith, H.
SWITZERLAND.
Basle—Merian, Prof. P. Geneva ( Celigny)—Gordon, L. D. B.
Berne—Studer, Prof. B. Neuchdtel—Desor, E
Geneva—Favre, Prof. A. Zurich—Heer, Rev. Prof. O.
Pictet, Prof. F. J. Linth, A. E. von der.
TASMANIA.
Hobart Town—Gould, C. | Hobart Town—Milligan, J.
WEST INDIES.
Antigua—Gilbert, Rey. N. | Trinidad—Guppy, R. J. L.
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