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A araielien th Saree ee agen aaa a

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LACE

Ni 4 THE

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

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

VOLUME THE SEVENTEENTH.

1861. <
PART THE FIRST. SU ASAUS

é at:
PROCEEDINGS OF THE GEOLOGICA OEM wy ‘pe wy

LONDON :

LONGMAN, GREEN, LONGMANS, AND ROBERTS.

PARIS ;—FRIED. KLINCKSIECK, 11 RUE DE LILLE; BAUDRY, 9 RUE DU COQ,
PRES LE LOUVRE; LEIPZIG, T. 0, WEIGEL.

SOLD ALSO AT THE APARTMENTS OF THE SOCIETY,

MDCCCLXI,

List
OF THE

OPFFICHRS

OF THE

GEOLOGICAL SOCIETY OF LONDON.

RARARR-E ARR An

Elected February 15th; 1861.

President.
Leonard Horner, Esq., F.R.S. L. & E.

Wice-BrestVents.

Prof. John Morris. Prof. John Phillips, M.A., a .D
Sir R. I. Murchison, G.C.St.S., F.R.S.& L.S. G. P. Scrope, Esq., M.P., F.R.S.

Secretaries.

Prof. T. H. Huxley, F.R.S. & LS.
Warington W. Smyth, Esq., M.A., F.R.S.

PFovretqn Secretary.
William John Hamilton, Esq., F.R.S.

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

COUNGCIL.
John J. Bigsby, M.D. Sir R. 1. Murchison, G.C.St.S., F.R.S. & L.S.
Sir Charles Bunbury, Bart., F.R.S.& L.S. | Robert W. Mylne, Esq., F.R.S.
Earl of Enniskillen, D.C.L., F.R.S. Prof. John Phillips, M.A., LL.D., F.R.S.
William John Hamilton, Esq., F.R.S. Major-General Portlock, LL.D., F.R.S.

Joseph D. Hooker, M. De F.R.S. & L.S. Joseph Prestwich, Esq., F.R.S.
E.

Leonard Horner, Esq. “9 F. R.S. L. & G. P. Scrope, Esq., M.P., F.R.S.

Prof. T. H. Huxley, F.R.S. & L. . Warington W. Smyth, Esq., M.A., F.R.S.
John Lubbock, Esq., F.R.S. & LS. Thomas Sopwith, Esq., M.A., F.R.S.

Sir Charles Lyell, F.R.S. & L.S. Alfred Tylor, Esq., F.L.S.

Edward Meryon, M.D. Rev. Thomas Wiltshire, M.A.

Prof. W. H. Miller, M.A., F.R.S. S. P. Woodward, Esq.

Prof. John Morris.

Assistant-Secretarp, Librarian, and Curator.
T. Rupert Jones, Esq.

Clevk.
Mr. George E. Roberts.

Pim eee

TABLE OF CONTENTS.

PART I.—ORIGINAL COMMUNICATIONS.

Page
Bropi®, The Rey. P. B. On the Distribution of the Corals in the
Mi tseeee PADS tC LS) Cechoevacrs sper avole lyons teraices aceaacdonee Pcisncystoiyenetse 151
Bunsury, Sir C. J. F., Bart. Notes on a Collection of Fossil Plants
from Nagpur, Central India. @Waths ope latess)iar tester crac 325
Ciarke, The Rev. W. B. On the Relative Positions of certain
Plants in the Coal-bearing Beds of Australia..,,............ 304
Dawson, Dr. J. W. Note on a Carpolite from the Coal-formation
Ct COTS IORNOOSS Sh omic doen ODN ma Onan DA pow Mie ca Goo tis 525
——. Onan Hrect Sigillaria from the South Jogeins, Nova Scotia.
PeNtiorerdxedlall itr igters eisleswierdiacatialtetoranensuctewbey ienare ate asics Nepura ygcl ak §22
—. Onan undescribed Fossil Fern from the Lower Coal-measures
GigNova Sc Oulase |e VDStraActsll Sarita eis e neil. auicicrc iy ween 5
Drew, F., Esq. On the Succession of Beds in the “Hastings
Sand” in the Northern portion of the Wealden Area ...,.... 271
Dykes, J. W., Esq. On the Increase of Land on the Coromandel
(Ons PASO RL Goan oo ac AN so be a nine moweto som hbo - 553
Everest, The Rey. R. On the Lines of Deepest Water around the
ES TLETSUMS Less eas EA NISLEAC al Pare tectchevots stotse ote) achetsters «ou ofol oltlous 081 ces 534

Fisuer, The Rey. O. On the Denudation of Soft Strata. [Abstract.] 1

Fontan, M. A. On two Bone-caverns in the Montagne du Ker at
Massat, in the Department of the Ariége. [Abstract.] ...... 468

Fores, D., Hsq. On the Geology of Bolivia and Southern Peru.
(CW. ith 3 Plates. buted o-aeo cenaaey cece riblonn Osea oh in ERP IRIS NIG BA. 0

Getnir, A., Esq., and Sir R. I. Murcuison. On the Western
Isles ad Western Highlands of Scotland .............. 171, 232

GusneR, Dr. A. On Elevations and Depressions of the Earth in
NoxiipAnnierica ma PMotid Sedalia. aj.ccsantsnolaaterty ek cs srs ele 381

TABLE OF CONTENTS.

Page
Gre@ory, F. T., Esq. On the ey of a part of Western Aus-
VENI Gin ocgooobobooG DOG OdUhOCGDUMGo DOH oDDoCR DDC CC SCC 475

Harkness, R., Esq. On the Rocks of portions of the Highlands of
Scotland South of the Caledonian Canal; and on their Hquiva-

lents im the North) ofireland\ 3): 2.) 0s sels iene otete reer 256
Harey, J., Esq. On the Ludlow Bone-bed and its Crustacean
Remainss q(Wath alate.) 9.1... «stein. cle tn ietetie a i-ietteritneet 542

Hecror, Dr. J. On the Geology of the Country between Lake
Superior and the Pacific Ocean (between the 48th and 54th
parallels of latitude), visited by the Government Exploring Ex- ~
pedition under the Command of Captain J. Palliser (1857-

1SGO)s > @Wathia Plates) ita.) cisiectas i alelaelseletelsveleis aie 388
Histop, The Rev. S. On the Age of the Fossiliferous Thin-bedded
Sandstone and Coal of the Province of Nagpur, India ........ 346

Huxury, Prof. T. H. On a New Species of Macrauchenia (M.
Bolumensis). (With a Plaite:)y vss etcmiere ors ernie) storey eet rererenaens 73

——. On Pteraspis Dunensis (Archeoteuthis Dunensis, Roemer). .. 163

+—. Onsome Reptilian Remains from Bengal ................ 362
JamrEson, T. F., Esq. On the Structure of the South-west High-
lands\of Scotland <i. cs.. cue sens cle cei eestaeiehslla trae 138
JEFFREYS, J. Gwyn, Esq. On the Corbicula (Cyrena) fluminalis,
geologically considered. iAbridged.j| 2 e102. cies netets tenets 473
Joass, The Rey. J. M. On the Occurrence of Old-Red Fishes at
Eidderton-in Ross-shire... scie0%. s/s <n 00 sitjeloeiee eee 593

Kirxsy, J. W., Esq. On the Permian Rocks of South Yorkshire,
and on their Paleontological Relations. (With a Plate.) .... 287

MircHett, The Rey. H. On the Position of the Beds of the Old

Red Sandstone developed in the Counties of Forfar and Kin-
Carding, Scotland... sisi sin ove ain inlo wise alelasl lel evermore eee 145

Moors, C., Esq. On the Zones of the Lower Lias and the Avicula
contorta' Zone: (With 2'Plates:) <0). ..06)s sine os slecstlsleeleteRene 483

Mourcutson, Sir R. I, and A. Grnxte, Esq. On the altered Rocks
of the Western ielanda of Scotland, and the North-western and
Central Highlands; with an Appendix by Sir R. I. Murcuison. 171

On the Coincidence between Stratification and Folia-
tion in the Crystalline Rocks of the Scottish Highlands ...... 232

Murray, C., Esq. Notice of the Occurrence of an Karthquake on
the 20th of March, 1861, in Mendoza, Argentine Confederation,
South America. [ Abstract. ] nein Bie aloreats oleate cloneiatie ea 553

Nico, J., Esq. On the Structure of the North-western Highlands,
and the Relation of the Gneiss, Red Sandstone, and Quartzite
of Sutherland ‘and Ross-shire...) 0.0 vae ss 2s eee 85

Prayratr, Capt. R. L. On the Outburst of a Volcano near Edd,
on the African Coast of the Red Sea. [Abstract.]) <= pci 552

TABLE OF CONTENTS.
Page

Powrt®, J., Esq. On the Old Red Sandstone Rocks of Forfarshire. 534

Prestwicu, J., Esq. Notes on some further Discoveries of Flint
Implements in Beds of Post-Pliocene Gravel and Clay, with a
few suggestions for search elsewhere .......seeeseeceecees 362

—. On the Occurrence of the Cyrena fluminalis, together with
Marine Shells of Recent Species, in Beds of Sand and Gravel over
Beds of Boulder-clay near Hull ; with an account of some Borings
and Well-sections in the same District

ooeseer se eee eee eee 8 8

Rickman, C., Esq. On the Sections of Strata exposed in the Exca-
vations for the South High-level Sewer at Dulwich; with
Notices of the Fossils found there and at Peckham. [Abstract.] 6

Saumon, H. C., Fsq. On the Occurrence of Large Granite Boulders,
at a great depth, in West Rosewarne Mine, Gwinear, Cornwall . 517

Satter, J. W., Esq. Note on the Fossils found in the Worcester

ands ereford: Railway, Cuttings’. ./. sees te + leliels) ole leis 161
——. On some of the Higher Crustacea from the British Coal-

NIGERUTNES do mens Sen Om oor eed om emNo Hnmn tole moco.clein ence 528
——. On the Fossils, from the High Andes, collected by David

Horbesmlisgen i Cras.) (Wath 2 Platess)) Vijsrsrucia weleisiseisluerersiels 62
Scort, M. W. T., Esq. On the “Symon Fault” in the Coalbrook-

dalerCoal=tiel ds a@Wathy apelates)\« tie aly sate oleic! ale) steelers) stelaiane 457
SmiTHe, J. D., Esq. On the Gravels and Boulders of the Punjab.

WWAMDStrac i llees CMa cre nels sae tacele hcteedes niet einia heel uerch neneo: 163
Symonps, The Rey. W.S., and A. Lampert, Esq. On the Sections

of the Malvern and Ledbury Tunnels (Worcester and Hereford

Railway), and the intervening Line of Railroad; with a Note

on the Fossils by J. W. Satter, Esq., F.G.S. ........+- 5660 Oy
Wuirtaxker, W., Esq. On a Reconstructed Bed on the top of the

Chalk, and underlying the Woolwich and Reading Beds...... 527
—, On the “Chalk-rock,” the Topmost Bed of the Lower Chalk,

in Berkshire, Oxfordshire, Buckinghamshire, &c. ............ 166
ASTSETITEI I] BS ONE 3 6b Geto ac aCe AO oO OG GEC ETO ES RE 5 i
PMEDREV CT SHEEP CUTE SS a ietev nates iets crcl casa slolateteiiep slic sieeve io! dietaveteca’ XXX1
Wisimoieboreieny Members) e'.. <crsiiteieroreycla cies tis exele le ailskorsi «i eatele slinie 0508
List of the Wollaston Medalists .................6% suit are cucmeuneat Xx1

Donations to the Library (with Bibliography) .. xii, 114, 241, 369, 554

EXPLANATION OF THE PLATES.

PLATE ; Pace
GroLocican Sknrcu-M ar oF PART or BOLIVIA AND PERU—SECTIONS
IE Across Prru AND BontviA—GENERAL SECTION ACROSS THE

II. AnpDEs oF Perv anv Bottyia (according to D’Orbigny, Pissis,
III. and D. Forbes), to illustrate Mr. David Forbes’s paper on
\ Bolivia and Peru.......,..... aise idteleais ie tastacteatastnateetent to face page 62

IV. | Fosstns rrom tie Anpzs, to illustrate Mr. Salter’s paper on
V. Bolivian Hossils, .cccseessoasenslasencucisenenatenatenatycadelne Seaeetemeeeeeeee 73

VI. Fosstz Bonzs rrom Bottvia, to illustrate Mr, Huxley’s paper on
Macranchenta Bolvurensts ides astce scene sn cen oe eece eee ee eee eee ee 84

VII. Prrnuran Fossins rrom Yorssurre, to illustrate Mr. Kirkby’s
paper on the Permian Rocks and Fossils of South Yorkshire ... 325

VALU ))
TX. | Fossm Prants rrom Centra InprA, to illustrate Sir Charles J. F.
Xx. Bunbury’s Notes on a Collection of Fossil Plants from Nagpur,

XI. Central’ Tdiias co iiens «cevesserles si onenercave ns ssiee saleieeeier serene eeeeeeet 346

aT

XIII. Gronocrcan Sxetcu-Mars or A pArt or NortH AMERICA AND OF
Vancouver Isnanp, AND Secrions, to illustrate Dr. James
Hector’s paper on the Geology of the Country between Lake
Superioriand the Pacific Ocean) oe .-cererescacsas doncareseeceenesert

388

XTV. Mar or A part or THE COALBROOK-DALE COAL-FIELD, to illustrate
Mr. Scott’s paper on the “ Symon Fault ”’ in the Coalbrook-dale

Moal?Feldysioncacat cask wun eaecails soeans aoe aCe R OREO ee 457

XY.) Ruztic Fosstts, to illustrate Mr. C. Moore’s paper on the White
XVI. Taas and -Auzerla contoria AON ..svc-daranp esse ons aeee acne eaeieceee 5

XVII. AsTACODERMATA FROM THE LupLow Bone-pep, to illustrate
Mr: Harley’s paper on -Astacodenma......<.1..-scsvaceceeenssaebeseaeh

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. (28.)
AUD. “enoadoccoboseoancocarcodeeHeCooea Seco as| RELMIAN essen:
Boliviana Binennis. PL We tio Wikcsoscaoos Lower Silurian..
Melocactus. Pl. v.f.9............ Lower Silurian..
provoscidea. Pl.v.f.10 ......... Lower Silurian..
(CHES WAG Gi Uecdscesooondsce ood) LHBHIS 6 csoo8ceoac0s
Cantar @)p LAG Site 1 Acacodocdagcocences Trias ees hechoss
Cruziana Cucurbita. Pl.v.f. 4-6 ...| Lower Silurian..
Unduani. Rlovete 7, 8 )<0c..e .....| Lower Silurian..
Cyclopteris (Aneimiles) Acadica ...... Lower Coal-
measures.
Fern, Rhizomeof (2). Pl. xii. f. 3... \
Glossopteris (?). IAL 3% 1858} ooco000s0 |
(yp bs nie Desenae pocogdonnene |
— Browniana, var. ‘Anevnenlbstiony |
TPG Catto s eG) cbodeneono cosiccooooasa teres || paiag >
Browniana, var. Indica. PI. 7 | Frias ?........+0.
Willis th thee cenonngononcbsocddeaoDdded
leptoneura. Pl.ix.f. 1- hee dadaee
musefolia. Pl.viii.f.6 ......
SULICL Om tales XontenO mts ilestanecs
Naiadita acuminata (?) .........ceseseeee Rhetic .........
Neggerathia? Hislopti. Pl. x. f. 8) Jodo) JUMEIS 2 cogasounses
Pachytheca spheerica ..... ndesgooudoass00d Old Red and
Upper Silurian
Pecopteris (2). Pl. ix. £.6-8.......0006 Mnias een cnenews os
Phyllotheca Indica. P\.x. f. 6-9, and
IA Sati I Pecooocgan hacobcacobsonez0KK66r (DTS Beoonbasonece
— (roots). Pl. xi. f. a eal INTER cece ddooosee
STUUILIPEE TETQUBIEE coesconecacapabocoonsnds Coal-measures .

.| South Yorkshire...! 309
IBXOHE, = Gooecdonoooe 72
Boliviale seecseceeee. 71
Boliviawiecceee: sense 71
Central India...... 332
Central India...... 340
Boliviaweereeeceenace 71
IBOKME). Goosodcaonee 71
Nova Scotia ...... 5

(340

333

| 333

Central India...... 4 329
326

330

329

331

Vallis, Rome ...... 512
Central India......| 334
Forfarshire and 146
Worcestershire 162
Central India...... 331
Central India...... 335
Central India...... | 338
.| South Joggins, 522

Nova Scotia. |

Vill

Name of Species. Formation. Locality. Page.

PLANT (continued).

Stem of a Plant. P1. xii. f.3............ ABER Bboadqnoaeced Central India......| 340
Tzeniopteris danzoides, McClell.? PI.

6 10174) GueagnosobocdcdpocudddoosaneamEHdoo0 HBTENS Boccocaboodec Central India......| 332
Trigonocarpum Hookeri. Woodcuts...| Coal-measures ..| Cape Breton ...... 525
NONEGTGS (Bs IALS Sis s64"" Kooeccocouooae ANTES Soosooosee ..-| Central India...... 341

FORAMINIFER.
Miliola pusilla............ss0.000+ +.eereeeee| Permian...,.....{ South Yorkshire...| 308

Coraniia. (2.)

Favosites (?), sp. Pl. iv. f.10 ......... Devonian ...... Oruro, Bolivia ...; 66
Montlivaltia, sp....c.0..06 saseeeeaaeeeecans IRINA © cagaoo0ed Beer-Crowcombe | 511
Bryozoa. (4.)

Acanthocladia ancepS.........seessesee
Retepora Ehrenbergi ..........00...00° . eee
Stenopora Mackrothi................. Permian .<.-2+..: South Yorkshire...| 307
Thamniscus dubius............0. pacKinod
Motiusca. (69.)
(Brachiopoda.)
Discina Townshendi ............00000.+-- | IBTESNG — ooogscoas Beer-Crowcombe.., 499
Orthis Aymara. Pl. iy. f.14............ | Upper Silurian..| Bolivia ............ 68
Bie. LA Gee BANG Ste peciaccconse | Upper Silurian..| Bolivia ............ 69
pb © LAIN BIG 7h ccaconscpaasnoodGen: ; Devonian ...... Oruro, Bolivia ...| 64
DENOM OMEN SPsit was. cacasneecavaccite> == | Upper Silurian..| Cotafia, Bolivia ... 69
Terebratula elongata .........sescessseee. phermianlccr<c--s0 South Yorkshire...| 306
(Lamellibranchiata.)
Anatina? precursor. PI. xvi. f.3...... | Rhetic ......... | Beer-Crowcombe..| 507
ORE TGS aolis 24 pocasotoanse ARERTO serococos Beer-Crowcombe..| 507
Arca? Brownii. Pl. iv. f.19, 20 ...... Upper Silurian..) Illampu, Bolivia... 69
Lycettii, Pl. xvi.f.7 ..-...00 | 501
Avicula contorta. Pl. xv. f.10...... 499
solitaria. Plo xvst. Wy sns- a. - 499
Axinus cloacinus. Pl. xv. f.16...... LS eB Pearocco- Beer Cray cote 502
concentricus. Pl. xy. f. 19-21 503
— depressus. Pl]. xv.f.17......... ) : 503
dubs) pelewaisk Woes. Bermianysracshes South Yorkshire...| 305
elongatus. Pl. xv.f.18.........++- Rheetic 0-00... Beer-Crowcombe..| 503
Cardiomorpha Pallasi.................s0- Bermianveesreeses South Yorkshire...| 304
Cardium Rheticum. Pl. xv.f. 28...... hweticgeress-cee Beer-Crowcombe..| 504
Ctenodonta (Nucula), sp. Pl. iv. f. 18.| Upper Silurian..) Bolivia ............ 69
Cucullella, sp. Pl. iv. £.17...00c.0+...0.. Upper Silurian..| Illampu, Bolivia... 69
Cyrene (Corbicula) fiuminalis............ Pilvocenereanas=- Kelsey Hill, York-| [ 446

shire. 473

Name of Species.

1x

Formation.

Locality.

(Lamellibranchiata) ee

Cexvilliarantiquasccenscceccsccescseaseee
Ksenatophacamincecsscecseicescseectes
ornata. Pl. xv. f. 8
precursor, El xvits Gy Jesccccese
Leda speluncaria...............++. pa0000800
Titei. Pl.xv. f.25
Lima precursor.
IMIGYOROGOM RUMELENS, goscoonosecsenscoHKonobe
Modiola minima. Pl. xv. f. 26,27 ...
Myacites striato-granulata. PI. xvi.

1is dL. GebobdoaaasupsroouacaicaEsEaescancotcs

eee ee se heoetooes

eee ecceec Co egronsccccce

Myophoria postera. PI. xvi. 8-190..

| Rheetic

tev eeevee
eeerssoee
evevescee
eoores eee

Rhetic .........
Rhetic .
Permian .........
JHINGRAN] ~ Goodcooos

Permian .........
Rheetic

eoorescece

Mytilus Hausmanni.................. pubdoo _| Permian BANS hors
Ostrea fimbriata. Pl. xvi.f.24 ...... IRIMESING. cooadoboe
interstriata. Pl. xv.f.25......... Rheetic .........
Pecten Valoniensis. Pl. xvi. f.6 ...... Rhetic--seces-t
Placunopsis Alpiva. PI. xvi. f. 4,5 )
Pleurophorus angulatus. Pl. xv.
% NW, 118}. Soconssacooanonsoebcscoonsode
elongatus. Pl. xv.f.14,15 ... +| Rhetic .........
Pteromya Crowcombeia. Pl. xv.
POO OMas elites cciee retinas de nsleaisecsiae |
simpler, P). xv. f.24 .......+. )
( Gasteropoda.)
Cerithium constrictum. P\.xvi £.13. )
cylindricum. Pl. xvi.f.15 ...
decoratum. Pl. xvi.f.14......
— Rheticum. Pl. xvi.£.16 ...... A ae
Chemnitzia Henrici(?). Pl.xvi.f.12.
=== (isi, LAL saytio tte Wh Gooaéoseccee
IRoessletinesccsnemeeeencersdseceecees Bermianieer cece
Chiton Loftusianus,..........-+..sse.sese0- Permian .........
Rheticus. Pl. xvi. f. 28, 29 .. podo0e Rhetic \ econ...
Cylindrites elongatus. Pl. xvi f. 20...) Rheetic .........
Susiformis. Pl. xvi. f.18......... ITEBTG Gooood600
CGO, Valo Sie it MS) ccogecona000006 INEAHO Gasocodos
oviformis. Pl. xvi.f. 21 ......... IRERHG — do5o00000
Dentalium Sorbyi .......0........0 ooo0d|| LEGMTMEN Sooscoo90
Natica minima? PI. vii. f. 7, 8 ......... Permian .........
Oppelit. PI. xvi. f.17 ...cccsesese IRIMEABG _covccanae
Patella (vel Pileopsis?) .....sseccecsseeee Upper Silurian
Rissoa Leighi. PI. vii. f. 1-6...;........ Permian .........
Straparollus Suessiz. Pl. xiv. f.2-5...| Rheetic .........
PMATENTOS cooacondoceq66qG000080000 ..| Permian .........
Trochus nudus. Pl. xvi.f.22 ......... Rheetie ........-
Waltgomie, — 12tbsoi. tke 2B naocop04000e INDERHG. cooboadios
Asie Oa) INENOVINS Socgsoconoodocosqonaeocado6 Permian .........
Tarritella Altenburgensis. Pl.vii.f.9,10 | Permian ..... 9000

(Nucleobranchiatum.)

Bellerophon, Sp. s.scceeves piatesietelaiste

So oeenee

Vallis.
Stoke-St.-Mary ;
Vallis.

Beer-Crowcombe

Beer-Crowcombe

Vallis, Frome
Beer-Crowcombe
Beer-Crowcombe
Beer-Crowcombe
Beer-Crowcombe

Beer-Crowcombe

Beer-Crowcombe

Beer-Crowcombe
Beer-Crowcombe

| Upper Silurian | Ulampu, Bolivia ...|

South Yorkshire...
South Yorkshire...
Beer-Crowcombe..
Beer-Crowcombe..
South Yorkshire...
Beer-Crowcombe..
Beer-Crowcombe..
South Yorkshire...
Beer-Crowcombe..

Beer-Crowcombe..|
South Yorkshire...
Beer-Crowcombe,.
South Yorkshire...
Wallis sseceescececius
Beer-Crowcombe ;

South Yorkshire...
South Yorkshire...

eeceee

South Yorkshire...
South Yorkshire...

Millepaya, Bolivia
South Yorkshire...

South Yorkshire...

South Yorkshire...
South Yorkshire...

Page.

70

Name of Species. Formation. Locality. Page.
( Cephalopodon.)
Nautilus Preiesle beni qrensssesceersclns sree (ePexmian\enc ener | South Yorkshire...| 297
CIRRIFEDE.
Pollicipes Rheticus. Pl. xvi.f.30 ...| Rheetic .........| Vallis, Frome ...... 512
Crustacea. (25.)
Anthrapalemon Grossarti. Woodcuts,| Lower Carboni-| Lanarkshire ......{ 530
f. 1-4. ferous. 530
(Palzocarabus) dubius. Wood-| Coal-measures | Coalbrook Dale ...
532
cuts, f. 6, 7.
4 Gis VOWGKIIS Ie Boccecsonancsocased| [oo -poDsoG00G0d4q0006 Lanarkshire ...... 530
Astacoderma bicuspidatum. P\. xvii. ) ( Ludlow& Norton} 549
6 7A Bn ts He |
declinatum. PI, xvii. £.9 ...... | Tudlow seers 551
planum. PI. xvii. f. 18-20 ... Ludlow& Norton) 552
— remiforme, Pl. xvii. f. 17...... ae: Ludlow & Norton) 552
fain bee EY cape Upper Silurian’ |> tudiow lata 550
—— spinosum. Pl. xvii. f.16 ...... udlowitenneseses 551
— terminale. Pl. xvii.f.1 & 14. Ludlow .....---- 549
—— triangulare. Pl. xvii.f. 5...... Ludlow ......... 551
undulatum. PI. xvii. f. 11-13. Ludlow & Norton} 551
Beyrichia Forbesiit. Pl.iv.f.13 ...... Upper Silurian | Illampu, Bolivia... 67
Cypris liassica(?) ....... nocoo non estescisss LSEESRVO. ongonose. Beer; Taunton ;) 512
Vallis.
Cythere (Bairdia) plebeia ............... Bennie nveremsieta: South Yorkshire...| 308
—— Schaurothiana ............. onipatces Benmianie serene South Yorkshire,.,| 308
(Cytherideis) Jonesiana.......... ee | P@nmianic.s sense South Yorkshire...| 308
Bishhevia MINNA sey ecacerceasaa san cesacesnc IME AAOS Adtincance Vallis, Frome ...... 512
Homalonotus Linares. Pl. y.f.1,2...| Upper Silurian | Mlampu, Bolivia... 66
SA7Mo TAREE RY nancodedsonoassacanse Upper Silurian | Ilampu, Bolivia.. 66
Karkbya Permiana ocsweecsecaceersensneene IRS ATTEN copsscone South Yorkshire...| 308
Paleocrangon socialis. Woodcut,f. 8.) Lower Carboni-| Fifeshire............ 533
ferous.
==) cosonoaenocbeconsnponeadocasanacnods Millstone-grit,..) Yorkshire ......... 533
Ehayps (Cryphaus) Pentlandii. P\.iv.| Devonian ...... || Aygatchi, Bolivia 65
oe)
SS IE eS LY LAs tebessenascisonnes Devonian ...... Oruro, Bolivia 65
ANNELIDA.
Annelide-tubes (2) .s...ee0e00e cqncon6600% Permian ......... South Yorkshire...| 309
Tentaculites Saienzit. Pl. iv. f.12...... _ Upper Silurian | Illampu, Bolivia .. 67
Supremuse Pe liiVate Uc. ssaeas <5 | Upper Silurian | [llampu, Bolivia... 67
WOrM-DUITOWS) casceescesesss+-secnemnacia | Upper Silurian | Bolivia ....... Arnie 68
INSECTA.
Carahidai(®)) Rigesscsyaehe ene eepesteaee isBhietic eck | Vallis, Frome ......| 513

Xi

Name of Species. | Formation. Locality.
PIscEs.
Pteraspis. Woodcut ............cseeeeees Devonian & Up-| Germany & Britain
per Silurian.
IDMINGMSIS. - coocdosooaesaads eerie vee Devonian ...... Lifel & Wassenach
Sargodon tomicus. Pl. xv.f.1......... | Rheetic .........| Beer-Crowcombe ;
Vallis.
SGUAlOLAIA, seceescseaecctaseceeseeeceseetees Rhetic .........| Beer-Crowcombe ;
| Vallis.
MamMMaALia,
Human Tooth. Weodcut,f.3 ......... Pliocene ......... Massat, Languedoc
Macrauchenia Boliviensis. Pi.vi. ...| Pliocene .......- Corocoro, Bolivia
MIsceELLANEOUS.
Blintllinplements) assc<csseesencneees .».-.| Pliocene ...,..++. Suffolk, Kent, Bed-!

fordshire.

Page.

470
73

363

Page

”

9

ERRATA ET CORRIGENDA.

Part I.—PRocrEEDINGS.

5, line 11 from bottom, for 22 read 23.
10, after line 5 from top énser¢ Sulphate of soda...10:97.
» line 8 from top, for 98°56 read 99°53.
46, line 16 from bottom, for ramos read ramo.
69, line 15 from bottom, znsert u. before sp.
125, line 8 from bottom, for Inzessdorfer read Inzersdorfer.
234, line 15 from top, for Mr. Sharpe read Mr. Sharpe’s paper.
237, in the last note but one, for p. 127 read pp. 20, 127.
358, line 17 from top, after But znsert as.
405, line 19 from top, after from énsert the.
417, line 13 from bottom, for blue-clay shale vead blue clay-shale.
448, line 5 from bottom (in the note), for in read on.
455, last line, for their read thin.
504, line 15 from top, for Prruroporvs read Punuroruorvs.
511, line 6 from top, for SrraparoLus vedd STRAPAROLLUS.
528, after the fourth paragraph, add,—

Whilst this paper was in the press I heard from Mr. Prestwich that
in a well near Waterloo Bridge, which passed through the beds from
the London Clay to the Chalk, the latter rock was found to be in a
rubbly or disturbed state to a depth of at least 20 feet below the Thanet
Sand.—W. W.

529, line 5 from bottom, for advantage read appendage.

531, last line, dele the ? after Palgocrangon; and at the end of the line
add—c. Enlarged.

€

533, line 12 from top, for long read short.

Part I1.—Misce..anzovus.

Page 30, line 2 from top, for Jonxuar read SonkuAr.

GEOLOGICAL SOCIETY OF LONDON.

ANNUAL GENERAL MEETING, FEB. 15, 1861.

REPORT OF THE COUNCIL.

In laying their Annual Report before the Geological Society of Lon-
don, the Council have much pleasure in congratulating the Fellows on
the ‘generally prosperous condition of the Society.

The number of new Fellows elected during 1860 was 35, making,
with four previously elected, whose fees were paid in 1860, an in-
crease of 39. During the same year the Society has had to regret
the loss by death of 19 Fellows.

One Foreign Member has been elected in lieu of one deceased.
The number of extraordinary Members has been reduced by the
death of one personage of Royal Blood and five Honorary Members.

The total number of the Society at the close of 1859 was 907 ; at
the close of 1860, 922.

The excess of Expenditure over Income during 1860 has been
£120 11s. 11d. This excess has been brought about by the occur-
rence of the following unusual items:—a donation of £50 to Mr.
Nichols, the Society’s late clerk, in consideration of his long ser-
vices; and £100 for the additional Number of the Journal, which it
was agreed to print in order to bring up arrears of publication.

The Council have to mention the handsome donation of 50 gui-
neas by Mr. Tylor, towards defraying the general expenses of the
Society.

The Funded property of the Society amounts to £4350 in Con-
sols, besides £500 of the Greenough and Brown Bequests, invested
temporarily, making in all £4850.

The Council have to announce the completion of Vol. XVI. of the
Quarterly Journal, and the First Part of Vol. XVII.

A revised List of the Fellows has also been printed and circulated.

In order to aid in the re-arrangement of the Museum, a second
VOL, XVII. a

iL ANNIVERSARY MEETING.

temporary Assistant was engaged at the recommendation of the Spe-
cial Museum Committee,—a step which has greatly assisted the pro-
gress reported by the Museum Committee.

The Council have to report that on the resignation of the office of
Clerk by Mr. Nichols, they considered it due to his long services to
present him with a sum of £50 ; and determined to recommend to the
General Meeting to award him a further sum of £70, making up one
year’s salary.

A great number of Candidates having presented themselves for the
post thus vacated, the Council, after a careful examination of testi-
monials, have bestowed the appointment on Mr. George E. Roberts.

In conclusion, the Council have to report that they have conferred
the Wollaston Medal on Professor Bronn, of Heidelberg, for his long and
successful labours in aiding the progress of geological science in ge-
neral, and more particularly for the assistance he has afforded to the
progress of Paleeontology, as evidenced in his ‘Index Paleontologi-
cus,’ and especially in his later work on the “ Laws of the Develop-
ment of the Organic World ;” and the balance of the proceeds of the
Wollaston Fund to M. Daubrée, of Strasbourg, to aid in the prosecu-
tion of synthetic experiments, similar to those of which he has re-
cently given an account, and which he has intimated his intention of
continuing, with the object of throwing light upon metamorphic ac-
tion.

Report of the Library and Museum Committee.

Museum.

The Collections of Minerals and of Recent Shells have received but
few additions; and in the latter the places of certain genera still re-
quire to be filled up.

The re-arrangement and re-naming of the British Silurian col-
lection has been completed by Mr. Salter; and the specimens have
been furnished with new tablets and labels: they now occupy 50
drawers.

The Rey. T. Wiltshire is proceeding with the arrangement of the
Chalk Fossils in the Museum.

For specimens received since the last Anniversary, illustrating the
geology of the British Isles, the Society is indebted especially to A.
Geikie, Esq., F.G.8., J. Evans, Esq., F.G.8., and the Rev. R. Hunter ;
and a large collection of fossil bones from Shorncliffe, lately forwarded
by the War-Department, is worthy of particular notice.

The Foreign Collection has been enriched with numerous dona-~
tions, among which the Committee would especially invite the atten-
tion of the Society to a valuable series of rock-specimens from Meissen,
and another from the Vosges Mountains, presented by the President:
the latter series, having been carefully selected and named in accord-
ance with the descriptions of M. Delesse, form an important typical
collection. They have also to notice Mr. Bennett’s Trilobites from
Newfoundland, Mr. Mallet’s Volcanic products from Italy, and va-

ANNUAL REPORT. lil

rious foreign specimens presented by Mr. Hamilton, F.G.S., the
Hon. Mr. Marsham, F.G.8., Mr. Purdon, F.G.S., and the Rey. 8.
Hislop.

Besides the above, a suite of Norwegian rocks and minerals, a do-
nation from His Excellency Count Platen, and a large collection of
fossils from Bordeaux (named by M. Deshayes), presented by Sir
Charles Lyell, deserve particular mention.

A new cabinet has been supplied for the use of the Upper Museum,
as recommended by the Special Museum Committee.

Grounding their views on an elaborate and valuable catalogue
prepared by Mr. Horner, of all the contributions from all countries,
the Special Museum Committee, at their Meeting on the 25th of June
last, resolved that the arrangement to be adopted shall be geogra-
phical, subordinate to which the fossiliferous specimens shall be in
stratigraphical order, and that the non-fossiliferous and eruptive
rock-specimens belonging to each geographical subdivision shall
follow the fossiliferous specimens. The Committee think it their
duty, in referring to this subject, to call especial attention to the
continuous labour and great zeal of the President, who, in superin-
tending the re-arrangement, has given his constant personal attend-
ance to the details of the business, and during the past year has
spent several hours of stated days in every week in actual work in the
Museum.

A thorough re-ordering upon the above plan has involved a mul-
tiplicity of details in the transfer from one cabinet to another, in the
rejection of useless specimens, 1n cleaning and labelling specimens and
drawers; notwithstanding which, under the almost daily superin-
tendence of the President, much has been accomplished in the ar-
rangement of the European collections.

These now occupy no less than 48 cabinets, containing 336
drawers ; and of their contents a very valuable and detailed cata-
logue has also been formed by Mr. Horner. They comprise—

Ist. The geographical arrangement of the countries of Europe,
with subdivisions in some—as France and Germany.

2nd. Under the head of each country, an account of the several
groups of specimens belonging to it, with the names of
the donors.

3rd. As the object of a geologist in examining"our foreign col-
lections may often have reference to a comparison of the
rocks or fossils of different districts, columns have been
prepared for references to facilitate such comparisons.

Mr. Horner’s catalogues are so constructed that future contribu--
tions can be at once added under their proper heads. It is to be
hoped that similar catalogues will accompany our collections from the
grand divisions of Asia, Africa, North America, South America, and
Australia. But the chief part, not only of the European, but also of
other collections, excepting some portion named by Mr. Horner, re-
quire naming, and are on that account defective, both rock-speci-
mens and fossils; and to this important subject the attention of the
Society is invited, in the hope that some othersamong the Fellows,

a2

lV

ANNIVERSARY MEETING.

possessed of competent knowledge, will come forward to aid in en-
hancing the usefulness of these valuable collections.
With the view of suggesting to volunteers the examination of par-
ticular groups, as also of reminding the Fellows of the variety and
extent of these collections, the following list is appended of several
series of fossils in the European collections which require naming :—

Fossils in the Foreign European Collections.

Formation.

Newer Pliocene,

or Pleistocene.
”

)
Plvoceneiaermenine

oP)
”)

”
Miocene nnick ses

loceneyatsis Siakeisalet

Sweden. Uddevalla, Opslo, and Stromstadt .

Lower Rhine. Loess, near Bonn ..........
Spain and Portugal. Gibraltar ............
Belguim. AMtWeL)). 0. + be er ora
Eastern France. Bones from Vesoul ......
Spain and Portugal. Lisbon..............
Sicily, Malta, and Gozo. Palermo, &e. ....

Central France. Touraine..... «de bodravtall open
Southern France. Bordeaux...... Rc 3
Spain and Portugal. Lisbon, &e...........

Spain and Portugal. Gibraltar, Alicant, Car-
thagena and Mula, and Totana in the Pro-
vince of Murcia ..... AIO aC aI6 al oletevattata

Spain and Portugal. Granada .......... 46

Steily, Malta, and Gozo. Malta and Gozo ..

Belgium. Brussels, Kunroot, Fauquemont,

Dati burp o-sy ahve es i sieieuahow exer oie AG 6
Lower Rhine. Brown-coal, near Boon sees
Northern France. Cassel ...........
| Western France. Hauteville, Dep. Manche .
|Central France. Paris Basin ....... ita

|\Central France. Bones from Auvergne . oe
Southern Prance: Biaritz 5... 5020+ 54 cle
Spain and Portugal. Murcia, &. ........

Northern Iialy. Monte Bolea ....... oie
Alpine Country. Glarus, Seefeld ..........
\Alpine Country, Flaming. nc) koe elas
| Western Germany. Mayence ............

\Adustria. Santa Margarita, Neusiedel, Kron-
1 bahay (GEE ch lsd cia oe eee

ae af? Buda ic Stee Gea eee
|Turkey in Europe. Moldavia ............
. |Southern France. Aix in Provence ......

Spain and Portugal. Malaga, Catalonia, and
[ep LuASDOM \ .. s injs; onic aiebaceee aera ee
Sicily, Malta, and Gozo. Sicily ..... as NE
‘Northern Italy. Piacenza, Turin, Bassano,
| Asolo and Pessagno, Tuscany, and Piedmont
‘Southern Italy. Antium, Rome, Agnano

| Alpine Country .......... SAGO 3057905 -

No. of
Drawers,

ro)

poy
DWN OWNER bdoe

a
Co Or

py

i
he co CO oO > (ot ll ell oe COD OW eRe Oe hope

ANNUAL REPORT,

Fossils in the Foreign European Collections (continued).

Formation.

Tertiary, undeterm.| Western Germany. Wetterau, Mayence

of Turkey in Europe. Bulgaria ............
> Grecian Archipelago. Candia, Hubea ....
> Southern Russia. Volhynia, Crimea ......
op AUSiaSTINMeEMM Ate ea aes: Bidaaeans were
Cretaceous <7.1......|Denmank. isle of Maxoe)) eines 0. bs oe.
” Holland. Maestricht and Aix-la-Chapelle. .
” Belgium. Tournay, Louisberg, Kunroot,

Montigny, Ciply, Konigsberg, Fauque-

mont, Schneeberg, &c.

” Western France. Charante, Normandy, Cap
MOMELO Ve fc Re ear a oy aie as SUN ec te ere. Luana ltt
” Central France. Meudon, Seine et Oise....
” Spain and Portugal. Lisbon, Leira, Portugal
” Alpine Country. Mont de Fis, Neuchatel,

OVROM EE wel sr scecrsue vr skeieetene cts ;
” Northern Germany. Essen, “Rheten, near
iElanover, meat Groslar Scciny. ac icl-telslele oer
” Central Germany. Drocden ie pe
” Turkey in Europe. Bulgaria ........ Goo
op Southern Russia. WVolhynia ..............
Wealden ........|Northern Germany. Buckerberg, Oberkir-
chen; Stamimentrnys sree erates te elie
Jurassic (including | Northern France. Boulonnais ........ siahv

Liassic).

55 Western France. Normandy ............

7 Eastern France. Besancon ..........
” Eastern France. Haute Sadne, Sultz-les-
IBPHUIR) So rns Ga AMO DOG aan mai nInieS On Bee
” Spain and Portugal. Granada, New Castile,
BE Corsets coc aial Nee aca ata Mone se Meliss: Sele letauey gi abet
” Alpine Country. Switzerland ........ seats
of Southern Germany. Bavaria ............
” Southern Germany. Aalen in Wurtemberg .
; ” Southern Germany. Mohringen, &c. ......
Triassic ..........|Eastern France. Sultz-les-Bains...........
op Central Germany. Thuringia ............
op Southern Germany. Mohringen, &e. ......
op Southern Germany. Stuttgart, Baden......
Secondary, undet....|Austivd. Viennals aohseaea sede ycieen «
” Turkey in Europe. Dobrutcha............
56 Jonna Tian, Ans eRmInn sobs 606 ao0bo60 60
is Southern Italy. Near Naples Bt evcAMiara ieee
5r, Southern Russia, \(Crimea\. 6.06. .6. +. 4:
” Alpine Countnay. | secteldiae nee. seer.
PEenmiianie ite (cyte Northern Germany. “Klein Neundorf......
” Western Germany. Wetterau............ |

” Central Germany. Mansfeld, Roseneck .

Parbonit crousiets, 1 SpeZen Gelman oe ie eo eee ao
” TB CLOTUA ae OLICT OE tates ite Ace Rare ete
op Lower Rhine. Rhenish Provinces ........

No. of
Drawers.

COR HS WW Re or

tH :
CHW OHH REE EE EDN DNHOWW FP HER He Hee FP BIO ©

bo

‘W1 ANNIVERSARY MEETING.

Fossils in the Foreign European Collections (continued),

Formation. oe

Carboniferous ....|Northern France. Boulonnais ..........., 1
” Spain and Portugal. Serra de Bussaco eel anal
” Northern Germany. Westphalia, Harzgebirge| 2
” Northern (Russia eek cui wot eee. aera 3
Deyonian ........ Lower Rhine. Rhenish Provinces ........ 23
on Northern France. Boulonnais ............ il
op Northern Germany. Westphalia.......... 1

» Western Germany. Dillenberg and Wissen-
: | chet: ls Nees OO ER VIL OA Rh co's 6 6
Silvia « iscsi Sweden. Vainnekulle, Gothland .......... 5
” Norway. Christiania, Malmoe, &c......... 5
- Lower Rhine. Rhenish Provinces ........ 23
op Western France. Normandy .......... ae 1
om Cenipal Hrance.\ Aneeray) \ip.iine scene 1
” Spain and Portugal. Oporto and Bussaco . 3
a SORGUIUG IM AA juls aia ua CR ee i!
” Northern Germany, Harzgerode.......... i
” Northern Germany. Wissenbach ........ 1
” Eastern Germany. Bohemia ............ 1
op Northern Russia, Volhynia ,..--..-..09=: 1
Paleozoic ...... 5% Northern Tialy.; Tuscany. .\. gcse: : slecians it
or Southern Russia, Crimea ,,...- sce 1
Miscellaneous ....|Central France. Auvergne .............. 1
Ae Alpine Country... Lynglv, ys ade sclaautemetee 1
” Grecian Archipelago incicisia\o,-lere eect it
or Southern: Busseg 4 sadheny duis vores eee iL

Tabrary.

Many new books and pamphlets have been acquired during the
past year, both by gift and purchase. For the latter purpose £100
of the Greenough and Brown Bequest-fund were expended on various
works, with which it was deemed desirable to enrich the Library.
Among them may be cited Hamilton’s ‘Campi Phlegreei ;’ Walters-
hausen’s ‘Aitna’ and ‘ Island ;’ Quenstedt’s ‘ Cephalopoden,’ ‘ Jura,’
and ‘ Handbuch ;’ Eichwald’s ‘Letheea Rossica ;’ Junghuhn’s ‘ Java;’
Kaup’s ‘ Urweltliche Siugethiere ;’ Gervais’s ‘ Paléontologie Fran-
caise ;’ Heer’s ‘ Tertiiir-Flora der Schweiz ;’ and D’Alton and Bur-
meister’s ‘ Gaviale’.

Many of the books and pamphlets have been bound, and with the
periodicals have been placed partly in the old, and partly in the new
Library-cases, which have been added in accordance with the recom-
mendation of the Library Committee of last year.

A new alphabetical Supplemental Catalogue has been published,
comprising nearly 3000 titles of books, pamphlets, and maps received
in the years 1856-59, including those bequeathed by Mr. Greenough,

ANNUAL REPORT. t vil

A copy of this Catalogue has been pasted in the leaves of the refer-
ence-catalogue in the Library, and the press-marks attached. Other
additions to the reference-catalogue have also been made, including
an alphabetical list of periodicals. There being now three separate
printed catalogues (1846, 1856, 1860), and three separate alphabet-
ical lists in the Catalogue of Reference, it is desirable that the whole
should be incorporated into one alphabetical catalogue for reference.
Nearly 400 titles.of books and pamphlets received or purchased during
1860 have been entered into an additional cataloguein MS. The
Maps have been lately re-arranged, and a reference-catalogue com-
pleted to the endof 1859. The contents of the portfolios of Sections,
Diagrams, Views, &c., have also been supervised, and catalogued in
MS.

The Assistant-Secretary reports that he has received much and
well-sustained assistance, chiefly in the Museum, and in preparing
era for the Evening Meetings, from Mr. Jenkins and Mr.

tair. oie
W. J. HAMILTON,
J. PRESTWICH,
J. MORRIS,
W. W. SMYTH.

Comparative Statement of the Number of the Society at the close of the
years 1859 and 1860. :

Dec. 31, 1859. Dec. 31, 1860.

Compounders :....245..5. UZ On Shh SMe aa 119
Resid etiiaiegt whine Ve: - 200 See ci ctca 214
Non —residentgiy: Wer Aan a. PG betes vin 531

vt las ; 844 864
Honorary. Members ...... 10 Eirias 5)
ioreign Members > o5)./ O0i0 a ek ele: Peso
Personages of Royal Blood.. 3-63 ......... 3—58

907 922

Vill ANNIVERSARY MEETING.

General Statement explanatory of the Alteration in the Number of
Fellows, Honorary Members, &c. at the close of the years 1859
and 1860.

Number of Compounders, Residents, and Non-residents,
Decemberns3le 185944 Biase cree epee eee 844
Add Fellows elected during former ) Residents .... 2
years, and paid in 1860 .. \ Non-residents . 2— 4
Fellows elected and paid in } Residents.... 14

US CO Maer eeeie haley Meio aoe Non-residents 21—35
39
883
Deduct Compounders deceased. ............:.20-0-00 al
Residents BO Taian RES Sie ie SPs BERR eee 2
Non=residents) 55 ees aad os a ace eee 16
_— 19
Total number of Fellows, Dec. 31st, 1860, as above...... 864
Number of Honorary Members, Foreign Members, and 63
Personages of Royal Blood, Dec. 31st, 1859 ..
Add Foreign Member elected during 1860.............. 1
64
Deduct Foreign Member deceased ............-2000- if
Hlotiorary Members jy.) (5s..5 eis eyes 5
— 6
As'above:s «<< 58

Number of Fellows liable to Annual Contribution, as Residents, at the
close of 1860, with the alterations during the year.

Number‘at the’ close’ of 1859225. ...52 «cae 6 see eee 200
Add Elected in former years, and paid in 1860........ 2
Elected’ and paid in 1860), -40).. 2)... See 14
Non-residents who became Resident ............ 11

— 27

227.
Deduct Deceased... Os os Sane os 2 ag es 2 ee eee 2
Became Non-resident... ./; ......2sseee eee 11

—— 13

As above:... on 214

ANNUAL REPORT. ix
DecEAseD FELLOWS.

Compounders (1).
Earl Cawdor.

Residents (2).

H. G. Bowen, Esq. | Sir Charles Fellows.
Non-residents (16).

W. Anstice, Esq. F. Downing, Esq.

W. Atkinson, Esq. R. G. Kallaby, Esq.

Dr. G. Buist. F. Looney, Esq.

Lieut.-Gen. Sir H. E. Bunbury, P. J. Martin, Esq.
Bart. Rev. Baden Powell.

Sir A. Caldcleugh. Karl of Tyrconnel.

J. Craig, Esq. Rev. R. N. Wallace.

Dr. J. G. Croker. W. Wills, Esq.

M. Dawes, Esq.

Foreign Members (1).
Prof. J. F. L. Hausmann.

Honorary Members (5).

Dr. Emerson. Dr. Hincks.
G. Hill, Esq. C. Keogh, Esq.
Dr. C. Skene.

The following Persons were elected Fellows during the year 1860.

January 4th.—Stephen Harlowe Harlowe, Esq., 2 North Bank, St.
John’s Wood; the Rev. S. W. King, Saxlingham Rectory, near
Norwich ; and David Llewellin, Esq., C.E., Glyn Neath, Glamor-
ganshire.

18th.—James Poyntz McDonald, Esq., Kingsdown Parade,
Bristol ; Wiliam Purdon, Hsq., C.H., Punjab; and James Winter,
M.D., Hampstead.

February 1st.—Thomas Pease, Esq., Westbury, Gloucestershire.

29th.—William Smith, Esq., C.E., Salisbury Street, Adelphi ;
and C. A. Sanceau, Esq., F.C.8., Blackpool, Lancashire.

March 14th.—The Rey. T. G. Bonney, M.A., Fellow of St. John’s
College, Cambridge; and the Rev. Henry Eley, M.A., Broomfield
Vicarage, Chelmsford.

28th.—His Grace the Duke of Marlborough ; and W. P. Jer-
vis, Esq., Northwick Terrace, Maida Hill.

April 18th.—Edward Brainerd Webb, Esq., C.E., 34 Great George
Street, Westminster; Spencer Herapath, 19 Sheffield Terrace,
Lena and Owen Bowen, Esq., 4 Great Queen Street, West-
minster.

x ANNIVERSARY MEETING.

May 16th.—Frederick Wollaston Hutton, Esq., Lieut. 23rd R. W.
Fusileers, Royal Staff College, Sandhurst; John James Lundy,
Esq., Primrose Bank, Leith; R. Farmer, Esq., the Hill, Hornsey ;
William Drury Lowe, Esq., Locko Park, Derby ; Arthur Beevor
Wynne, Esq., of the Geological Survey*of Ireland; and James
Wyatt, Esq., Bedford.

30th.—Mark Fryar, Esq., Lecturer on Mining, &c., at the
Andersonian University, Glasgow; and Francis Duncan, Esq.,
Lieut. R.A., Halifax.

June 13th.—George Angus, Esq., 3 Harcourt Buildings, Inner
Temple; Herbert T. James, Esq., Drumkeeran, Co. Leitrim; and
Henry Ward, Esq., the Oaklands, Wolverhampton.

November 7th.—William T. Blanford, Esq., of the Geological Survey
of India; the Rey. Thomas Bigsby Chamberlin, Kirton in Lind-
say, Lincolnshire; James Sparrow, Esq., Cymmau Hall, near
Wrexham; and Richard Fort, Esq., Read Hall, Whalley, Lan-
cashire.

21st.—Major Robert Jones Garden, 63 Montagu Square; and
Lieut. Robert Home, R.E., Royal Staff College, Sandhurst.

December 5th.—William Salmon, Esq., Ulverstoke, Lancashire ;
Peter Higson, Esq., one of H.M. Inspectors of Coal-mines,
Broughton, near Manchester ; John Spencer, Esq., Bowood, Wilts ;
Alexander R. Binnie, Esq., C.E., 7 Upper Lansdowne Terrace ;
George James Eustace, Esq., Arundel House, Brighton; F. D. P.
Dukinfield Astley, Esq., Dukinfield, Cheshire, Arisaig, W.B., and
67 Eaton Square; and Thomas Baxter, Esq., Cathedral School,
Worcester.

—— 19th.—The Rey. A. Deck, of the Royal Military College, Sand-
hurst ; Charles Rooke, Esq., Scarborough ; and the Rey. William
Lister, Bushbury Vicarage, Wolverhampton.

The following Personage was elected a Foreegn Member.
M. H. Milne-Edwards, Jardin des Plantes, Paris.

The following Donations to the Musrum haye been received since the
last Anniversary.

British Specimens,

A series of thirty-six specimens of trappean rocks from Arthur’s
Seat, Edinburgh ; presented by A. Geikie, Esq., F.G.S,

Specimens of peat and shells from Stirlingshire ; presented by the
Earl of Selkirk, F.G.S.

A series of plaster-casts of Cystideze ; presented by J. Mushen, Esq.

Specimens of fossil-wood from Woburn; presented by John Evans,
Esq., F.G.S.

Specimens of pseudomorphs of salt in Keuper Sandstone, from Deer-
hurst ; presented by T. R. Jones, Esq., F.G.S.

Skull of Cat in stalagmite, from a bone-caye in 8, Devon; presented
by C. Babbage, Esq., F.R.S.

ANNUAL REPORT. xi

Specimens of Corals from the Lias; presented by the Rev. P. B.
Brodie.

Specimens of Fossil Ferns from Wyre Forest Coal-field; presented
by Mr. George E. Roberts.

Slab of Old Red Sandstone from Mill of Ash; presented by the Rev.
J. Hunter.

Specimens of Wealden Unios from Tunbridge Wells; presented by
W. J. Hamilton, Esq., For. Sec. G. 5S.

A Collection of fossil Mammalian Bones from Folkestone ; from the
War-Department, through Capt. G. H. Gordon, R.E., Shorncliffe.

Foreign Specumens.

Specimens of Hollow Pebbles from the Leitha-Kalk; a suite of 156
rock-specimens illustrative of the geology of the Vosges Moun-
tains; and specimens of Porphyries and Pitchstones from Meissen ;
presented by Leonard Horner, Esq., Pres. G.S.

Specimens of Paradoxides Bennettii, from Newfoundland; presented
by — Bennett, Esq.

Specimens of Nemertites Strozzii from Tuscany, and some Carboni-
ferous fossils; also a series of Tertiary fossils from Bordeaux ;

_ presented by Sir C. Lyell, V.P.G.S.

A suite of Volcanic Rocks from Italy; presented by R. Mallet, Esq.,
F.G.8.

Specimens of Rocks from Tuscany ; Devonian fossils from the Bos-
phorus; Agate-specimens from Oberstein ; and specimens of Opal
from Konigswinter; presented by W. J. Hamilton, Hsq., For.
Sec. G.S.

Specimens of nodules with Fish-remains from Brazil; presented by

the Hon. R. Marsham, F.G.S.

Specimens of Carboniferous fossils from the Punjab; presented by
W. Purdon, Esq., F.G.S.

Specimens of Mya arenaria, from Nieue Deep, Holland; presented
by J. G. Jeffreys, Esq., F.R.S.

Slab of flexible Sandstone, from Narnoul, India; presented by C,
Gubbins, Esq.

A series of eighty-five specimens of rocks, minerals, and ores, from
Sweden and Norway; presented by His Excellency Count Platen,
Swedish Ambassador.

Specimens of Coal from Sah-Koh, Persia, collected by Mr. Mackenzie,
H.M. Consul for Gilan ; from the Foreign Office, by order of Lord
John Russell.

Specimens of fossils, coprolites, and bones from Nagpur, India; pre-
sented by the Rev. 8. Hislop.

Specimen of silicified wood from the Banda Oriental; presented by

- J. P. Harries, Esq.

xii ANNIVERSARY MEETING.

CHarts AND Maps PRESENTED.

Sheet 32 (Scotland) of the Geological Survey of Great Britain ;
Sheets 101-112, 119-121, 128-205 (Ireland) of the Geological
Survey of Great Britain; Sheet 12 (England); Sheets 107, 108,
six-inch, of Lancashire ; and Nos. 2, 3, 4, and 5, Horizontal Sec-
tions (England) of the Geological Survey of Great Britain ; pre-
sented by the Director-General of the Survey.

Kisenbahn-Karte von Deutschland, und den angrenzenden Lin-
dern, bearbeitet von Dr. Reden und E. von Sydow ; presented by
Leonard Horner, Esq., Pres. G. 8.

Carte Géologique et Coupes Géologiques de la partie de Sud d’Ural
Montagnes, composée par MM. Meglitzky et Antipoff; presented
by the authors.

Sheet No. 1 (Melbourne) of the Geological Survey of Victoria; pre-
sented by that Survey.

Drawings, §¢., presented.

A coloured print of H. B. de Saussure, and three of Glacier-travelling ;
presented by T. J. Laing, Esq., F.G.S.

A drawing of Ceelorhynchus rectus, and of Pristis Lathami; pre-
sented by Leonard Horner, Esq., Pres. G. S.

Two engravings of Flint-weapons found at Hoxne in Suffolk ; pre-
sented by John Evans, Esq., F.G.S.

The following Lists contain the Names of the Persons and Public
Bodies from whom Donations to the Library and Museum have been
received since the last Anniversary, February 17, 1860.

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

Auckland. New Zealand Govern-
ment.

Basel, Natural History Society of.

Berlin, Geographical Society of.

——, German Geological Society
at.

, Royal Academy of Sciences
at.

Berwick. Naturalist’s Field Club.

Boston (U. 8.), Natural History
Society of.

Bordeaux, Société Linnéenne de.

British Government.

Brussels. L’Académie Royale des
Sciences.

Caen. Socicté Linnnéenne de
Normandie.

Calcutta. Geological Survey of
India.

Bengal Asiatic Society.

Cambridge (Mass.). American
Academy of Arts and Sciences.

Canadian Government.

Cassel. Natural History Society
of Upper Hesse.

Cherbourg, Société des Sciences
Naturelles de.

Copenhagen. Royal Danish Aca-
demy of Sciences.

Cornwall. Royal Cornwall Poly-
technic Society.

ANNUAL REPORT,

Cornwall, Royal Geological Soci-
ety of.
, Royal Institution of.

Darmstadt. Geological Society of
the Middle Rhine.

, Geographical Society of.

Dublin, Geological Society of.

, Royal Irish Academy at.

Edinburgh, Royal Society of.
——, Royal Physical Society of.

Frankfurt, Senckenberg Natural

History Society of.
(Kentucky). Geological
Survey of Kentucky.

Geneva. La Société de Physique
et d'Histoire.
Glasgow Geological Society.

Halle, Society of Natural Sciences
of.

, Saxon and Thuringian Na-
tural Society in.

Hanau. Natural History Society
of the Wetterau.

Heidelberg, Natural History So-
ciety of.

Hobart Town. Royal Society of
Tasmania.

India, Secretary of State for.
Towa, Geological Survey of.
, Government of.

Kentucky, Geological Survey of.

Lausanne. Société Vaudoise des
Sciences Naturelles.

Leeds, Philosophical Society of.

Liege, La Société Royale de.

Lisbon, Royal Academy of.

Liverpool. Lancashire and Che-
shire Historical Society.

, Philosophical Society of.
London. Geological Survey of
Great Britain and Ireland.

, Royal Astronomical Society

of.

xiil

London. Royal Asiatic Society of

Great Britain.

, Art Union of.

British Association.
——., Chemical Society of.
College of Surgeons of
England.

. College of Physicians of

England.

——. Royal Geographical Society.
Geologists’ Association.

, Royal Horticultural Soci-
ety of.

Institute of Actuaries of
Great Britain and Ireland.

. Institute of Civil Engineers.

Tnternational Statistical
Congress.

, Linnean Society of.
——., Mendicity Society of.
——,, Meteorological Society of.
——, Microscopical Society of.
——., Photographic Society of.
——., Royal Society of.

. Royal Institution of Great
Britain.

Ray Society.

. Societyforthe Encourage-

ment of the Arts.

, Statistical Society of.

——, Zoological Society of.

International Association
for obtaining a uniform Decimal

System of Measures, Weights,

and Coins.

Lyons, les Commissionnaires Hy-
drométriques de.

Madrid, Academy of Sciences of.

Manchester, Literary Society of.

Melbourne. Royal Society of Vic-
toria.

——. Geological Survey of Au-
stralia.

——, Government of.

Milan, Imperial Institute of.

Montreal, Natural History So-
ciety of.

Moscow, Imperial Academy of
Naturalists of.

“xiv
Munich, Academy of Sciences of.

Neuchatel, la Société des Sciences
Naturelles de.

New Haven (U.S.). Editor of

' American Journal of Science.

New York, Geographical and Sta-

' tistical Society of.

, State Library of.

New Vealand Government.

Offenbach, Natural History So-
ciety of.
‘Ohio, Board of Agriculture of.

Paris, l’ Académie des Sciences de.

, Dépot Générale d’ Annales

des Sciences Naturelles a.
L’Ecole des Mines.

. Museum d’Histoire Natu-

_ relle.

Pesth, Academy of Sciences of.

Philadelphia, Academy of Natu-
ral Sciences of.

American Philosophical

Society.

American Association for

the Advancement of Science.

. Franklin Institute of Penn-
sylvania.

Puy-en-Velay, la Société d’Agri-
culture et Sciences du.

St. Louis, Academy of.

ANNIVERSARY MEETING.

Stockholm, Academy of.

St. Petersburg, Imperial Aca-
demy of.

, Mineralogical Society of.

Strasburg. Museum d’Histoire
Naturelle.

Stuttgart. Fatherland Natural
History Societyof Wurtemberg.

Somersetshire, Archeological and
Natural History Society of.

Toronto(Government of Canada),
Public Libr ary of.

Turin, Academy of Sciences at.

Tyneside Naturalists’ Field-club.

Vienna, Geological Institute of.
, Imperial Academy of.

United States, Government of.

Washington. Patent Office.

——. United States War Depart-
ment.

Smithsonian Institution.

Wiesbaden. Natural History So-
ciety of the Grand Duchy of
Nassau.

Yorkshire, Philosophical Society
of.

—— (South). Viewers’ Associa-
tion.

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

since the last Anniversary.

Adhémar, M. G.

American Journal of Science and
Art, Editor of the.

Anea, Baron.

Ansted, Prof. D. T., F.G.8

Antipoff, M.

Atheneum Journal, Editor of the.

Babbage, C., Esq.
Bache, Prof. A. D.

Barrande, M. J., For.M.G.S8.
Bennett, — Esq.

Bergh, H., Esq.

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

Bland, T., Esq., F.G.S.
Botfield, T., Esq., M.P., F.G.S.
Bouquet, M.

British Government.

ANNUAL REPORT. XV

Campiche, Dr.

Carpenter, Dr. W. B., F.G.8.

Chambers, R., Esq., F.G.S.

Chemist and Druggist, The Edi-
tor of the.

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

Critic, Editor of the.

Daubeny, Dr., F.G.S.
Daubrée, M.A.

Dayidson, T., Esq., F.G.S.
Dawson, Dr. J. W., F.G.S.
Delesse, M., For.M.G.S.
Deslongchamps, M. E. E.
Desnoyers, M. J.

Doué, M. B. de, For.M.G:S.
Duckworth, H., Esq., F.G.S.
Duff, P., Esq.
Dulau & Co., Messrs.
Eichwald, M. E. von.
Evans, J., Esq., F.G.S.

Fayre, M. A.

Forbes, J. D., Esq., F.G.S.
Forchhammer, Dr., For.M.G.S.
Foreign Office. :
Forrester, J. J., Esq., F:G.8.
Francis, Dr. W., F.G.S.
Freke, Dr. H.

Gabb, M., Esq.

Gaudin, M. C. T.

Geikie, A., Esq., F.G.S.
Geinitz, Dr. H. B., For.M.G.S.
Geologist, Editor of the.
Goppert, Dr. H. R., For.M.G.S.
Gosselet, M. J.

Grant, Dr. R. E., F.G.S.
Gubbins, C., Esq.

Hamilton, W. J., Esq., For. Sec.
G.S

Harries, J. P., Esq.

Hauer, Chev. K. v.

Haven, C. H., Esq.

Hawn, F., Esq.

Hébert, M. E.

Helmersen, Col. G. v.
Henwood, W. J., Esq., F.G.S.

Hislop, Rev. 8.

Hogg, J., Esq.

Holmes, F. 8., Esq.
Horner, L., Esq., Pres.G.S.
Hunt, T. 8., Esq.

Hunter, Rev. R.

Jeffreys, J. G., Esq.
Jeitteles, L. H.

Jervis, W. P., Esq., F.G.S.
Jones, T. R., Esq., F.G.8.

Hames Jee Kisqu rks GS:

Lane, C. B., Esq.

Laugel, M. A.

Lea, Dr. I.

Lindsay, Dr. W. L.

Literary Gazette, Editor of the.

London, Edinburgh, and Dublin
Philosophical M agazine, Editor
of the.

Longman & Co., Messrs.

Lyell, Sir C., V.P.G.S.

Mallet, R., Esq., F.G.S.

Mancow, M. J.

Marsham, The Hon. R., F.GS.

McAndrew, R., Esq.

Mechanics’ Magazine, Editor of
the.

Meglitzky, M.

Meigs, Dr. J. A.

Meyer, H. von, For.M.G.S.

Mining Review, Editor of the.

Mitchell, Rev. H.

Mohrenstern, M. G. 8. von.

Morris, Prof. J., F.G.8.

Morton, G. H., Esq., F.G.S.

Murchison, Sir R. I., V.P.G.S.
Mushen, J., Esq.
Newberry, J. 8., Esq. e

New Zealand ‘Examiner, The
Editor of the.
Nisser, P., Esq.

Oldham, Prof. T., F.G.S.
Ormerod, G. W. Esq., F.G.S.
Owen, D. D., Esq.

Owen, Prof. R., F.G.S.

XV1

Parker, W. K., Esq.

Parolini, Signor C. A.
Phillips, Prof. J., F.G.S.
Pictet, M. F. J.

Platen, His Excellency Count.
Purdon, W., Esq., F.G.S.

Quaritch, B., Esq.

Quarterly Journal of Microsco-
pical Science, Editor of the.
Quarterly Journal of theChemical

Society, Editor of the.

Ramsay, Prof. A. C., F.G.S.
Raulin, M. VY.

Readwin, T. A., Esq., F.G.S.
Reeve, L., Esq., F.G.S.
Rentzsch, Dr.

Roberts, G. E., Esq.
Roemer, Dr. F., For.M.G.S.

Scharff, Dr.
Selkirk, Earl of, F.G.S.

ANNIVERSARY MEETING,

Shumard, F.

Silliman, Prof., For.M.G.8.
Smyth, R. B., Esq., F.G.S.
Smyth, W. W., Esq., Sec.G.S.
Sorby, H..C., Esq., F.G.S.
Steindachner, M. F.
Stoliczka, M. F.

Studer, Prof. B., For.M.G.S.
Strozzi, M. le Marquis C.
Suess, Prof. E.

Swallow, G. B., Esq.

Tate, G., Esq., F.G.S.
Tennant, Prof. J., F.G.S.
Thomson, Prof. W., F.G.S8.

Verneuil, M. de, For.M.G.8.
Vivian, E., Esq.

Wallich, Dr. G. C., F.G.S.
War Department.

Zigno, Signor A. de.

List of Parmrs read since the last Anniversary Meeting,
February 17th, 1860.

1860.

Feb. 29th.—On the Classification of the Lower Lias of the South of

- England, by Dr. T. Wright, F.G.S.

March 14th.—On the occurrence of the Lingula ‘Crednert in the
Coal-measures of Durham, by J. W. Kirkby, Esq. ; communicated
by T. Davidson, Esq., F.G.S.

——_—-41 On the Rocks and Minerals on the property of the
Marquess of Breadalbane, in Perthshire and Argyleshire, by Carl
H. G.Thost, Esq.; communicated by Prof. Nicol, F.G.S.

March 28th.—On the so-called Wealden Beds and the Reptiliferous
Sandstones of Elgin, by Charles Moore, Esq., F.G.S.

Notes about Spitzbergen, by James Lamont, Esq.,

F.G.8.

Aprib 18th.—On the presence of the London Clay in Norfolk, as
proved by a Well at Yarmouth, by Joseph Prestwich, Ksq.,
Treas. G.S.

——_—— Ona Well in the Tertiary Sands and Clays at Bury
Cross, near Gosport, by J. Pilbrow, Esq. ; communicated by the
President.

On some Foraminifera from the Triassic Clays at

Chellaston, near Derby, by T. R. Jones, Esq., F.G.S., and W. K.

Parker, Esq.

ANNUAL REPORT. -XVil

1860.

May 2nd.—On the Physical Relations of the Elgin Sandstones, by the
Rey. W. 8. Symonds, F.G.S.

——___—-— On two newly discovered Bone-caves in Sicily; a
letter from Baron Anca to Dr. Falconer, F.G.S.

May 16th.—An outline of the Geology of Venezuela and Trinidad,
by G. P. Wall, Esq.; communicated by Sir R. I. Murchison,
WeE-Ges: |

——__———— On the Co-existence of Man with certain Extinct
Quadrupeds, by M. HE. Lartét, For. M.G.S.

May 30th.—On certain Rocks of Miocene Age in Tuscany, by W. P.
Jervis, Esq., F.G.S.

——__—_———. On the Ossiferous Caves of Gower, Glamorganshire,
by Hugh Falconer, M.D., F.G:S.

June 13th.—On the Bone-caves of Gower, Glamorganshire (in con-
tinuation), by Hugh Falconer, M.D., F.G.S.; with an Appendix
by Joseph Prestwich, Esq., Treas. G.S., on the Raised Beach of
Mewslade Bay, and the Existence of Boulder-clay in Cefn-y-bryn.

On the occurrence of Crag-shells beneath the Boulder-
clay of Aberdeenshire, by T. F. Jamieson, Esq.; communicated by
Sir R. I. Murchison, V.P.G.S.

—__—___—_——- On some small Fossil Vertebrze from near Frome, in
Somerset, by Professor Owen, F.G.S.

November 7th.—On the Denudation of Soft Strata, by the Rev. O.
Fisher, F.G.S.

—_——_— On an undescribed Fossil Fern from the Lower Coal-
measures of Nova Scotia, by Dr. J. W. Dawson, F.G.S.

——— On the Sections of Strata exposed in the Excavations
of the South High-level Sewer at Peckham and Dulwich, with
Notices of the Fossils found there, by C. Rickman, Esq, ; commu-
nicated by the Assistant-Secretary.

November 21st.—On the Geology of Bolivia and Southern Peru, by
David Forbes, Esq., F.G.S8.; with Notices of the Fossils, by Prof.
Huxley, Sec. G.S., and J. W. Salter, Esq., F.G.S.

December 5th.—On the Structure of N. W. Highlands, and the Rela-
tions of the Gneiss, Red Sandstone, and Quartzites of Sutherland
and Ross-shire, by Prof. James Nicol, F.G.S.

December 19th.—On the Geological Structure of the S.W. Highlands
of Scotland, by T. F. Jamieson, Esq.; communicated by Sir R. I.
Murchison, V.P.G.S.

On the Position of the Beds of the Old Red Sandstone
developed in the counties of Forfar and Kincardine, by the Rey.
Hugh Mitchell ; communicated by the Secretary.

1861.

January 9th.—On the Stratigraphical Position of certain Liassic
Corals, by the Rev. P. B. Brodie, F.G.S.

On the Malvern and Ledbury Tunnels on the Wor-

cester and Hereford branch of the West Midland Railway, by the

Rey. W. 8. Symonds, F.G.S8., and A. Lambert, Esq.

On the “ Chalk-rock” lying between the Lower and

Upper Chalk of Wilts, Berks, &c., by W. Whitaker, Esq., F.G.S.

VOL, XVII. b

Xvi ANNIVERSARY MEETING.

1861.

January 22nd.—On the gravel and boulders of the Punjab, by J. »D.

_ Smithe, Esq.

——_—_—— On Pteraspis Dunensis(Palwoteuthis Dunensis, Roemer), s
by Prof. Huxley, Sec. G.S.

February 6th.—On. the Altered Rocks of the Western and Central
Highlands of Scotland, by Sir R. I. Murchison, V.P.G.S., and A.

- Geikie, Esq., F.G.S.

After the Reports had been read it was resolyed,—

That they be received and entered on the int of the Meeting ;
and that such parts of them as the Council shall think fit be printed
and distributed among the Fellows.

It was afterwards resolyed,—

1. That the thanks of the Society be given to Sir C. Lyell and
Meir: General Portlock, retiring from the ‘office of Vice-President.
“2. That the thanks of the Society be given to Sir P. G. Egerton,
tik R. Godwin-Austen, Esq., W. Hopkins, Esq., and J. C. Moore,
Ksq., retiring from the Council.

After the Balloting-glasses had been duly closed, and the lists
examined by the Scrutineers, the following gentlemen were declared
to have been duly elected as the Officers and Council for the ensuing
year :—

OFFICERS.

—_@——_.

PRESIDENT.
Leonard Horner, Esq., F.R.S. L. & E.

VICE-PRESIDENTS.
Prof. John Morris.
Sir R. I. Murchison, G.C.St.8., F.R.S. & LS.
Prof. John Phillips, M.A., LL.D.
G. P. Scrope, Esq., M.P., F.R.S.

SECRETARIES.

Prof. T. H. Huxley, F.R.S. & L.S.
Warington W. Smyth, Esq., M.A., F.R.S.

FOREIGN SECRETARY.
William John Hamilton, Esq., F.R.S.

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

ANNUAL REPORT.

X1X

COUNCIL.

John J. Bigsby, M.D.

Sir Charles Bunbury,
E.R.S. & LS.

Earl of Enniskillen, D.C.L.,
eS:

Wilam John Hamilton, Esq.,
TEARS:

Joseph D. Hooker, M.D., F.R.S.
& LS.

Bart.,

Leonard Horner, Esq., F.R.S.

L. & HK.
iProie Won Huxley, ERS.
John Lubbock, Esq., F.R.S. &
LS.
Sir Charles Lyell, F.R.S. & L.S.
Edward Meryon, M.D.
Prof. W. H. Miller, M.A., F.R.S.

Prof. John Morris.

Sir R. I. Murchison, G.C.St.S.,
JT Gash Wa IS)

Robert W. Mylne, Esq.

Prof. John Phillips, M.A., F.R.S.

Major-General Portlock, LL.D.,
E.R.S.

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

G. P. Scrope, Esq., M.P., F.R.S.

Warington W. Smyth, Esq., M.A,,
ERS:

Thomas Sopwith, Esq., M.A.,
F.R.S.

Alfred Tylor, Esq., F.L.S.

Rey. Thomas Wiltshire, M.A.
'S. P. Woodward, Esq.

b2

LIST OF

THE FIFTY FOREIGN MEMBERS

OF THE GEOLOGICAL SOCIETY OF LONDON, 1y 1861.

Date of
Election.

Bis
1817.
1818.
1819.
1819.
1819.
1821,
1822.
1823.
1825.
1827.
1827.
1828,
1828.

1828.
1829,
1829.
1832,
1839.
1840,
1840,
1841.
1841.
1844.
1844,
1847,
1847.
1848.
1850,
1850.
1851.
1851.
1851.
181.
1851.

Professor L. A. Necker, Geneva.

Professor K. C. yon Leonhard, Heidelberg.

Professor Karl yon Raumer, Munich.

Professor G. Ch. Gmelin, Tubingen.

Count A. Breuner, Vienna.

M. Charles Lardi, Lausanne.

Sign. Alberto Parolini, Bassano.

M. Louis Cordier, Paris.

Count Vitiano Borromeo, Milan.

Professor Nils de Nordenskidld, .4bo.

Dr. G. Forchhammer, Copenhagen.

Dr. H. yon Dechen, Oberberghauptmann, Bonn.

Herr Karl yon Oeynhausen, Oberberghauptmann, Breslau.

M. J. M. Bertrand de Doue, Puy-en- Velay.

M. Léonce Elie de Beaumont, Sec. Perpétuel de l'Instit. France,
For. Mem. R. 8., Paris.

Dr. B. Silliman, New Haven, Connecticut.

Dr. Ami Boué, Vienna.

J. J. d’}Omalius d’Halloy, Namur.

Professor Eilert Mitscherlich, For. Mem. R. 8., Berlin.

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

Professor Adolphe T. Brongniart, For, Mem. R., S., Paris.

Professor Gustav Rose, Berlin.

Dr. Louis Agassiz, For. Mem. R. 8., Cambridge, Massachusetts.

M. G. P. Deshayes, Paris.

Professor William Burton Rogers, Boston, U.S.

M. Edouard de Verneuil, Paris.

Dr. M. C. H. Pander, Riga.

M. le Vicomte A. d’Archiac, Paris.

James Hall, Esq., New York.

Professor Bernard Studer, Berne.

Herr Hermann von Meyer, Frankfort on Maine.

Professor James D. Dana, New Haven, Connecticut.

Professor H. G. Bronn, Heidelberg.

Colonel G. von Helmersen, St. Petersburg.

Dr. W. K. Haidinger, For. Mem. R. 8., Vienna.

Professor Angelo Sismonda, Turin,

1853.
1858.
1854.
1854.
1856.
1857.
1857.
1857.
1857.
1858,
1858,
1859.
1859,
1860,

exo

Count Alexander von Keyserling, S¢. Petersburg,
Professor Dr. L. G. de Koninck, Liege.

M. Joachim Barrande, Prague.

Professor Dr. Karl Friedrich Naumann, Leipsic.
Professor Dr. Robert W, Bunsen, Heidelberg,
Professor Dr. H. R. Goeppert, Breslau,

M. E. Lartét, Paris.

Professor Dr. H. B. Geinitz, Dr esdene

Dr, Hermann Abich, S¢. Petersbur: I

Dr, J. A. B: Dealenselaniye Caen, |

Herr Arn. Escher von der Linth, Zur ich,

M, A. Delesse, Paris, =~

Professor Dr. Ferdinand Roemer, Breslau,
Professor Dr. H. Milne-Edwards, For.Mem.R.S., Paris,

AWARDS OF THE WOLLASTON-MEDAL

UNDER THE CONDITIONS OF THE “ DONATION-FUND”?

- WILLIAM HYDE WOLLASTON, MD. F.RS,,

- ESTABLISHED -BY

F.GS., &.,

“To promote researches concerning the mineral structure of the earth,
and to enable the Council of the Geological Society to reward those
individuals of any country by whom such researches may hereafter be

made,”—*“ such individual not being a Member of the Council.”
1831. Mr. William Smith. 1848. The Rey. Dr. W. Buckland,
1835. Dr. G. A. Mantell. 1849, Mr. Joseph Prestwich, jun.

1856.
1837.

1838.
1839.
1840.

1841,

1842.
1843,

1844.
1845.
1846.
1847,

M. L. Agassiz.

ae P. F. Cautley, -
Dr. H. Falconer.

Professor R. Owen...

Professor C. G. Ehrenberg.

Professor A. H. Dumont.

M. Adolphe T. Brongniart.

Baron L. von Buch.
ae Kk. de Beaumont.
M. P. A. Dufrénoy.

The Rey. W. D. Conybeare.

Professor John Phillips.
Mr. William Lonsdale.
Dr. Ami Boué.

1850.
1851.
1852.

1853.

1854.
18655.
1856.
1857.

18658..

1859,
1860.
1861,

Mr. William Hopkins. |
The Rev. Prof. A. Sedgwick.
Dr. W. H. Fitton.

; | M. le[Vicomte A. d’Archiac,

M. E. de Verneuil.

Dr. Richard Griffith.

Sir H. T. De la Beche.

Sir W. E. Logan.

M. Joachim Barrande.

| Herr Hermann von Meyer.
Mr. James Hall.;

Mr. Charles Darwin.

Mr. Searles V. Wood.

Prof. Dr. H. G. Bronn.

Income and Expenditure during the

INCOME.
: £635 (de Be “sii:
Balance at Banker’s, January 1, 1860.... 531 7 9
Balance in Clerk’s hands ....... LehGe te 9 1a 2
a el
Compositions received. 2. 5523352:ih¢ sta Fee ae 110 5 0
Arrears of Admission-fees ...:.......; 29-8.,0
Arrears of Annual Contributions ...... Cae OO
ae ea ee aD
Admission-fees for 1860 ........ Pe eee ¢ ca-bertee oe! yao
Annual Contributions for 1860............ vee eae 670 19 6
Dividends on 3 percent. Consols*. i). 2 scac+ sa see 1380 15 10

Publications :

Longman and Co., for Sale of Quarterly Journal

MERE) anoobhcocconopebeéc0suodaudoc ay) ie
SalevonEransactlons\aatsievaletataterell-leleiolelterate orate ey I
Sale of Proceedings ~- =>. -25..-- 00+. eresee Onis
Sale of Journal; Volso 1=6) <a cas-ecmeetel =< 914 0
os Wols.-7—leisssecate sac Neva 'stes5, yO GEO
iF Walesa UGE sd. etcdnewc'es Sle ames
+ WO Wi sceonccceadodouc 123) 10) 9
sale of Geological Map ........--...e-e0s ATs 50
Sale of Library-catalogues, including Dona-
tion from the Rey. C. Pritchard.......... 5 18 6
Sale of Alphabetical Catalogue .......¢.-.. OPSe0
Sale of Ormerod’s Index ............204- 2 4 0
—_———.. 312 4110
Journal-Gompositions .; 24.55. Ssae86 es eeen as tees y COS ORC
J

“

We have compared the Books and
Vouchers presented to us with these
Statements, and find them correct.

S. R. PATTISON,
Feb. 2, 1861. JOHN J. BIGSBY,

* Due from Messrs. Longman and Co., in addition
to the above, on Journal, Vol. XVI. ........ £63 12
Due from Fellows for Subscriptions toJourn. .. 63 8
Due from Authors for Corrections...........+. 713

\ Auditors.

£134 13

lol] mow

£2228 15

1

Year ending December 31st, 1860.

EXPENDITURE.
General Expenditure : 25 db efi lesb ds
AK ES| Matfer ercrecevelereicienoleiare cretevelctsveleiatersl «(c 53 0 8
Fire-Insurance ........ccsecsssccrecees 3.0 0
House-Repairs 2... .ccccvceccssccsecece 12 5 8
Karmituremerrcrerrisiciec seleleicielscicisiclercel --- 3818 9
Hine leerereyeteterietecitoielcsieieicicioietcloioricictereiareiaic 40 9 0
Tighe ise Acs oid asc u ee aaa as 34 0 2
Miscellaneous House: ~CXPeNS€S.. 2. ecccsee. 69 13 Il
Sfationery) ccc snulas sel meeie ce uiae 29 16 4
Miscellaneous Printing........... agueo ad 36 0 6
Meattor WMeetin ys) ants penile cicre crete ele.cls 15 110
——- 332 6 10
Salaries and Wages :
Assistant-Secretary ......00 cesses s eens 200 0 0
(UBER ascosgndoocanessasdascuo0 Bekstetels 108 15 0
Assistants in Library and Museum ........ 84 5 0
Porter.s..cese. SETAE AS BIS OCI REE 90 0 0
HIG USEMAIG EL M2e ee ee ee oe eee aed 40 0 0
Occasional Attendance....... sisters (cise 15 F:0
(CollGgine “ssocdecausundooduoote HoObonoE 24 5 0
—— 562 6 0
WabTAGVeete epee tc eee a escee bea ses Badihe) setae ale Wik aay) a4
Alphabetical Sipplementat Celee ue ge Pissoeese) Veto)
Witseunes sacs es scree Sh ese Ss ctveno cigs a: 43 12° 6
Diagrams at Meetings ........ seve soyer sgddedGoou jLe) (OM
Miscellaneous Scientific Expenses .............. See IC sinteuea
Donation (part) to Mr. Nichols ....... eessrssess, 00.0) 0
Publications :
Geological Map .........0. goadDd000 0000 5418 6
Proceedings and Abstracts .............. 10 7 6
danmal, Wales Ik Wo so oclboago0 asGoddKe 012 8
is WOR MANOS cogasoonsudonoob 1 9 0
Ks WOK ANUS Oeocacc6oudoboouo4 19 13 6
AT Viol XVI ashes ee eee 67612 7
763 13 9
Invested by Treasurer out of Journal-Composition .. 200 O O
ipalancerat) bankers Deco 1 S60) 4m ase ae 19 8 10
ibalaneeum-Clerk’s hands <2... .2se 6 S50 ees 15 3.6

£2228 15 1

| Estimates for .

INCOME EXPECTED.

Sait
Due for Subscriptions on Quarterly Journal account Sr |
: 40 0 O
sidered good) .......40. EUaSe loa tte slaneen caueeseecneg UES ae aR
Due for Authors’ Corrections .......- 50000000 Merron. 7 18.6
Arrears (See Valuation-sheet) ........sseeees iduawaaee ssedoosddaasees 119 15 QO
Ordinary Income for 1861 (estimated) :— Toul ee)
Annual Contributions, 213 Resident Fellows 67 ee
AES QS. crcccccssccccccocaccssccscessessssscsscerceas 101 oe
Annual Contributions, 30 Non-resident. Fel-
a7 DagO
lows at 14 2S. “ccoccceoes sangdpasdoagdane00Ge000000
i fills 4 Ov
Admission-fees (Supposed) .......cseeeeeeees soins oictoiatsteetne aera 200 0° 0
Compositions (supposed) ........seeeee. SpSsonaa00000c8 osesenoseenenll om OmmO
Dividends on 3 per Cent. Consols | ......seeeseees cocbscveeneceassoatlc tut 2mmO
Sale of Transactions, Proceedings, Geological Map, me -100 0 0
brary-catalogues, and Ormerod’s Index ......+sseeeseseeeere
Sale of Quarterly Journal): wesscccccsseessrescresesctenrcdceckanieaane 200 0 O
Due by Messrs. Longman and Co. in June ..........sceceseceeeeee 63 12 3

Portion of Mr. Greenough’s Bequest of £500, ordered by the
Council to be sold out on account of special Expenditure
incurred on Map, Library, and Museum during 1859 and
IYO) Sqncaandsco00d eer eeeecccccccacccsetences csneccsesscceerscscasocs 200 0 0

Further amount due from expenditure incurred } 10617 3
during 1860 in same account.......cseseereseeees

Special Expenditure during 1861 to be met out ) 300. 0 . 0

of the Bequest-fund -.....c..e.eceee etececeee censee
=== 406 17 3
£2332°14~0 |

JOSEPH PRESTWICH, Treas.
Feb. 11, 1861.

the Year 1861.

EXPENDITURE ESTIMATED.

eB Bo th. 28 Ah OA
General Expenditure :
. Taxes and Insurance ...... o6a000000¢ a “..- 40 0 0
House-Repairs, sere ss pices cece ce sice 00) a
Se ecial Expenditure .......... £100 ji 1) YO
TUK ~~ codao0 besa 0000 000000 00 bn OaGO DE 50 0 0
tHe cgnooabogabacose 90 05.000000 0000000000 35 0 0
Light | 2.2... eee ee es cece nsec cess cree eens 309 0 0
Miscellaneous House-expenses .......++- ---- 530 0 O
Stablonenygaycrrcyserecyavereteloktsveiateievevelapersiereneisvets ' 30.0 0
Miscellaneous Printing, including Abstracts.... 40 0 0
Tea for Meetings........ le te neseecee. --.-. 30 0 0 Bis
460 0 0
Salaries and Wages:
Assistant-Secretary ...... 6060000 socscrecess 200 0 0
Clak sooscabdocdqgcodsoonb obo DD Ou 0000 - 79 0 0
Mr. Nichols (remainder of donation) ........ 70 0 O
Assistants in Library ......escceccecesccece 81 0 0
EQIP oooobo oo oo do boo OD OGD 00Gb00000000 90 0 0
TOUSETAIG Metavelchererchersley etstoloi ekeyereoiojel= 10000000 40 0 0
Occasional Attendants ........ co ogsD00000 - 20 0 0
(Cokie sooo ooooonodo Hi ROR ae ihe te Bi al ete oo A OD)
602 0 0
Library : Ordinary Expenditure ..........0000. ese rOOn tOnnO Mie
D Special Expenditure* ............+. coadocn 60) @) ©
100 0 QO
- Museum: Ordinary Expénditure ............0e00e0. 50.0 0 ae
s Special Expenditure* ......c00...seee0000, 50 .0 '0
_————— 100 _0. 0-
DiacramsratyVlectMeS\e sac occsescncssseecscseeadecel smcsc seas osetcnan | OnuO) a On
Miscellaneous Scientific Expenditure .........0ssscccsssseerereeee 13 °O0 O
Publications: Quarterly Journal ............es0e00--- 650 0 0
mI Mransactionsy senses coekcceesees | LOU Or. 0
op Geological: Map, «special .expendi- ©

ture* ' PHOCCOCOP OG HHO LO TET BOC ORO ROH DE8SD 100 (0) (0) i i
ee ODD)

AB a: £2040 0 0

Balance in favour of the Society ...sssccccsscscesrsssseeessceeee 292 14 O-

£2332 14%: 0

_*® The “Special Expenditures” included in this Estimate
- refer to charges to be met out of the Greenough and Brown
Bequest-fund, should the Council consider, from time to
time, such expenditure advisable.

*suorjisod
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ayy Aq avak sig pasvarout heey os[e sey yy *Ayetoduia4
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‘ps F : *SINENAVG ee *SLd1GOayY

*LNQODDY wae

“PROCEEDINGS
AT THE

ANNUAL GENERAL MEETING,

151m FEBRUARY, 1861.

AwarD or THE Woxtaston Mrpat.

Arter the Report of the Council had been read, the President,
Lronarp Horner, Esq., F.R.S. L. & E., delivered to the Foreign
Secretary, Witt1am Joun Hamitron, Ksq., F.R.S., as representative
of Professor Bronn of Heidelberg, the Wollaston Medal, addressing
him as follows: —

_ Mr. Hamitron,—The Council: have awarded the Wollaston Medal
to Professor Bronn of Heidelberg, for his long-continued and suc-
cessful labours in-aiding the progress of geological science in general,
and more particular! ly for the dcsistates ie has afforded to the
progress of paleontology by his ‘Index Palsontologicus,’ and espe-
cially by his last work, on the “ Laws of Development of the Organic
World.”

. A very wide range of subjects is embraced ‘in his numerous publi-
eations, which extend over a period of nearly forty years. Among the
earler ones I may refer to his ‘ Travels in 1824-1827 in Switzer-
land, the South of France, and Italy,’ in which many important
topics of Natural History and Geology are treated of. These were
followed, in 1831, by a description of the Italian tertiary formations
and their fossil shells and other organic contents. I may next
mention the well-known ‘ Lethea Geognostica,’ which has gone
through three editions since 1834, and which was followed by those
most useful volumes called the ‘ Index Paleontologicus, or Review
of all known Fossil Organisms,’ prepared with the co-operation of
Professor Goppert of Breslau and of Hermann yon Meyer of Frank-
furt. The compilation of this work, however laborious, must have
been beneficial, not only to the public, but to the author himself, by
obliging him to study that vast store of materials on which he has
since generalized with so much originality and success in several
treatises on the philosophy of paleontology. It is impossible to

XXVIil PROCEEDINGS OF THE GLOLOGICAL SOCIETY,

overrate the importance of that work to the geological student, or
the difficulty of its compilation, in arranging and comparing the
numerous organic remains described by different persons in different
places, and in giving due precedence to the numerous synonyms
which have been introduced.

In relation to his theoretical speculations on the plan of creation,
as deduced from geological data, and from the present state of the
natural world, I may in particular advert to his treatise entitled
‘ Investigations of the Laws of Development of the Organic World,
during the period of the Formation of the Earth’s Surface,’ to which
a prize was awarded in the year 1857 by the French Academy,—the
subjects proposed having been, “ first, to examine, the laws of the
distribution of fossil organic bodies in the different sedimentary for-
mations, according to “the order .of their superposition ; secondly,
to discuss the question of their successive or simultaneous appearance
or disappearance ; and thirdly, to inquire into the nature of the
relations between the existing state of the organic world and its
anterior states.”” In that remarkable work we are presented with a
series of tabular’ views, exhibiting the numerical distribution of
fossil genera and species, both of plants and animals, as they appear
in the successive stratified formations of the earth’s crust, capable
of serving not only as statistical documents of the highest value to
illustrate a theory of the development of life, but also as a standard
to which future palzontologists may refer when they desire to know
the point which their science has reached in our time.._ In the same
work the Professor has endeavoured to show that a progressive
advance towards the perfection of animal and vegetable forms and
attributes has kept pace with a parallel and equally gradual improve-
ment in the external conditions of life, or in the habitable state of
the globe.

Professor Bronn supposes that there has been a passage from a
thalassic and insular to a continental state of the globe, in’ which
high mountain-chains and large areas of land separated by .inter-
yening seas have been’ formed, and .that during: those changes a
contemporaneous development of the organic world has been going
on, from the most simple and imperfect to-the more complex and
perfect—a progress equally displayed by plants and animals,—the
acotyledonous, for. example, having preceded the dicotyledonous
plants, and the marsupial mammals of the oolite having appeared
before the placental forms of the tertiary period.. This relation of
the continued improvement in the physical state of the: earth’ and
the concomitant changes inorganic life Professor Bronn calls the
terripetal law. Without pretending: to offer any opinion on these
difficult problems, to which my own studies have not been directed,
I. may observe that we, should be lost in the contemplation of the
multiplicity. of facts already accumulated respecting the past history
and present state of the organic and inorganic worlds, were they not
presented to us in a connected view by “the aid of some such bold
and: comprehensive’ theoretical speculations, which are the more
interesting when we consider their bearing on Mr. Darwin’s views,

ANNIVERSARY ADDRESS OF THE PRESIDENT. XX1X

since published, “On the Origin of Species,” which, though di-
stinect and independent, have a close connexion with the theories
which Professor Bronn has treated with so much ability.

Mr. Hamirton replied as follows :—

Mr. President,—It is with great satisfaction that I receive at your
hands the Medal which has been awarded to Professor Bronn by
the Council; and I shall have much pleasure in forwarding it to
my learned and distinguished friend, with whom I have been inti-
mately acquainted for many years, and whom I have always found
willing to impart his information in the kindest and most liberal
manner. You, Sir, have so fully expatiated on the merits of
Professor Bronn, that it is unnecessary for me to occupy the time of
the meeting in saying more on that subject ; I shall therefore con-
fine my observations to a brief notice of what Professor Bronn has
written to me in the letters in which he requested me to receive the
Medal for him.

In the first place, he has requested me to express his thanks to the
Council for the great honour done to him by this award—an honour
all the more remarkable in consideration of the many other distin-
guished individuals whose names were brought forward as candidates
on this occasion. He then observes, with regret, that he has no
practical field for his geological and paleontological exertions. He
cannot travel and make discoveries; he has not even the use of a
public collection ; and he is restricted to his own means, and these
are small. He trusts that, by his publication of the ‘ Index Pale-
ontologicus, and ‘ Lethzea Geognostica,’ he has given to others some
assistance in prosecuting more extensive studies ; and finally he ob-
serves that he has laid down the results of his own studies, in two
works, one of which obtained the prize offered by the French
Academy ; the other, entitled ‘The Gradual Progress of Organic
Life, from the Rock Islands of the Ocean to the Continents,’ is an
Appendix to the “ Law of the Terripetal Development of Organic
Life in Geological Time,” which he had established in the above-
mentioned Prize Essay. I may add that, as the result of these laws,
one of which is dependent on the outward conditions of existence,
and the other is the effect of an independent creative force, Professor
Bronn has endeavoured to show that in proportion as, first rocky
islets, then groups of islands, mountain-chains, and finally large
continents were raised above the level of the sea, a corresponding
progression of organic life from less to more perfect forms was
gradually called into existence.

In conclusion, I will only say, Sir, that, while again expressing
Professor Bronn’s sincere thanks for the distinguished but (as he
says) unexpected honour which has been conferred upon him by the
Council, I shall take the earliest opportunity of forwarding to him
this mark of the Council’s approbation of the eminent services:
which he has rendered to geological investigation.

XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

AWARD OF THE WOLLASTON DoNATION-FUND.

The President next addressed Sir Roperick Mourcuison, as the re-
presentative of M. Davsréz, in the following terms :—

Str RopEricx,—You are aware that the bequest of Dr. Wollaston
enables the Council each year to bestow a second mark of distinction,
but in another form, in order to show their sense of some valuable
service rendered to geological science, and generally to aid researches
in progress which involve considerable expense,—the sum at their
disposal being, however, by no means a measure of the value they
attach to the researches. On the present occasion, they have made
this award to M. Daubrée, Dean of the Faculty of Sciences at
Strasburg, Professor of Mineralogy and Geology in that Faculty, and
a Chief Engineer of Mines; and I have to request that, as his
personal friend, you will convey to him this testimony of the
interest we take in those his researches, which have hitherto been
attended with very important results. ;

The words of the award are these :—“ to aid in the prosecution of
synthetic experiments similar to those of which he has recently
given an account, and which he has intimated his intention of con-
tinuing, with the object of throwing light upon metamorphic action.”

But it is not only as an eminent chemical philosopher that M.
Daubrée has an extensive reputation in his own and in foreign
lands; he has long made valuable contributions to geology by other
works. His publications date from the year 1836; since which time,
besides sixteen memoirs on the analysis of minerals and other
subjects of chemical geology, we have had from him a Geological
Map of the Department of the Lower Rhine, accompanied by an
octavo volume of 500 pages with 111 figures, descriptive of its
geology and mineralogy ; ‘ Observations on the Ancient and Modern
Alluvia of a part of the Basin of the Rhine;’ ‘On the Erratic
Phenomena in the North of Europe and the Recent Movements of
the Land in Scandinavia ;’ ‘ Observations on the Quantity of Heat
employed to evaporate Water at the Surface of the Globe,’ and
‘On the Dynamic Force of the Running Waters of the Continents ;’
and no less than twenty minor memoirs on miscellaneous geo-
logical subjects, succeeded by his ‘ Observations on Metamorphism,
and Experimental Researches on some of the Agents which may
have produced it ;’ and lastly, his important work, a copy of which
he has recently presented to this Society, entitled, ‘Studies and
Synthetic Experiments on Metamorphism,’ to which I shall have
occasion to refer in the course of the address I am about to deliver.

Sir Ropertck Murcuison replied as follows :—

Sir,—I have listened with great satisfaction to what you have
said (and so well said) in relation to the meritorious services of
M. Daubrée, and I have a true satisfaction in being made the
medium of transmitting to him the proceeds of the Wollaston Fund.

ANNIVERSARY ADDRESS OF THE PRESIDENT, XXX1

I am convinced that on no preceding occasion have these proceeds
been awarded to a person who by his researches more completely
realizes the design and object of the illustrious testator.

Seeing that M, Daubrée is continuously engaged in the prosecution
of that ‘branch: of experimental science which! geologists most call
for, and knowing that he has already thrown ereat and important
light on some of the most occult processes of nature in the meta-
morphism. of rocks, I may take the liberty of saying that I hope
the notice we now take of such labours may be but the prelude to
our speedy enrolment of this distinguished man among the Foreign
Members of the Geological Society.

THE ANNIVERSARY ADDRESS OF THE PRESIDENT.

I congratulate you on the favourable position of the Society which
the report from your Council has presented to you. Although we
have to lament the deaths of many of our Fellows during the past
year, I have not to read to you such a melancholy list as you heard
from this chair at our last Anniversary, of the names of many of our
associates eminent in science taken away from us in a single year;
for our sorrow has been aggravated by the decease of but a few of
those from whom future valuable contributions to the advancement
of our science might have been looked forward to with confidence.

The Rey. Professor Baprn Powett died last June, at the age of sixty=
three. He took first-class honours at Oxford in 1817, became a Fellow
of the Royal Society in 1824, and in 1827 was appointed Savilian
Professor of Geometry in the University of Oxford, an office which
he retained to the time of his death. He was elected a Fellow of
this Society in 1837, and was a frequent attendant at our evening
meetings ; and, although chiefly known for his labours in physics,
and especially in Light and Heat, he contributed much, by a variety
of writings, to the general acceptance by the public of ‘the results of
geological investigations. He had worked but little at field-geology;
but his unusual grasp of mind and habits of industry enabled him,
whilst closely engaged in other branches of science, to keep pace
with the recent observations and current literature of geology,
especially on the great general questions in our science the most
attractive to a philosophical mind.

The fruits of these studies were embodied in numerous articles in
reyiews, and in a series of works devoted, in great part, to inquiries
into the relations between physical science and religion. Such were,
‘The Connection of Natural and Divine Truth, 1838;’ ‘ Essays
on the Spirit of the Inductive Philosophy, &c.,’? 1855; ‘The Unity
of Worlds and of Nature,’ 1856; ‘The Order of Nature,’ 1859.
In the latter work there is a most interesting sketch of the progress
of geology, from which I am tempted to quote the following ad-
mirable passage :—“‘ The evidence of the true influence and progress
of philosophical principles in this grand department of science—
grand in itself, but more transcendently so in relation to the

XXX PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

* cosmos,’ as carrying back the dominion of physical law through
the abysses of past time—in its earlier stages was found where
perhaps we might least have looked for it—among the Italian writers.
The mantle of Galileo descended, in some measure, on Vallisneri and
Moro, and more amply on Generelli, though a Carmelite monk.
We here perceive perhaps the first oreat advance in true philo-
sophical ideas of geology, and the anticipation and prototype of the
real inductive independent views of Hutton and Lyell, under the
vivifying influence of whose principles the English school of
geologists is but now beginning to cast off the lingering remnants of
its hereditary bondage to mystical paroxysms, occasional recurrences
of chaos and creation, subversions and renewals of the order of
nature, and miraculous originations of new species out of nothing—
in a word, the spirit of invoking the supernatural to cover our ig-
norance of natural causes*.”

His broad and liberal views, and his fearless assertion of the truths
to which he was conducted by reasoning on facts, exposed him to
the shafts of prejudice and bigotry, the more envenomed from the
fact of his being himself in Holy Orders. But, although conscious
that he was thereby putting a bar on his prospects of worldly ad-
vancement, he continued to the end to work steadily in the course
which his conscience dictated, satisfied that at a later day justice
would be rendered to his arguments. He was at the same time
ever ready to give to his opponents the same credit for that sincerity
of belief and honesty of purpose by which he, doubtless, felt he was
himself actuated, and to which we all know he might justly have
laid claim.

His lucid style, philosophical tone, and. extensive learning
secured for him, as a writer, the sympathy and support of ‘the
friends of intellectual progress, whilst his private friends had to
admire his constant readiness to assist and instruct, his lively in-
terest in and great acquaintance with most branches of knowledge,
his skill as a musician and draughtsman, and his unassuming kind-
ness of disposition. For many years he formed one of a small band at
Oxford who kept alive the study of the physical sciences} during a
season when they were not regarded with so much favour as at the
present day; and when, in 1850, he was appointed to be one of the
Oxford University Commissioners, he had the satisfaction of aiding
to introduce some of those modifications which have now given the
physical sciences a recognized position in the system of studies
adopted at the University.

Perer Jonny Martin, Esq., of Pulborough, Sussex, was elected a
Fellow of this Society in 1833, and died last May, aged seventy-four.
Established as a medical man in the Valley of the Arun, Mr.
Martin had two favourite holiday-studies, which he continually
pursued, as an antiqaarian and a geologist. Of his researches in the
history of the Roman Roads, and in other archeological subjects,
his antiquarian friends are well aware; and accounts of them have
* Order of Nature, p. 161.

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXili

been published. Of his geological studies there are records in the
Proceedings and Journal of this Society, in the ‘ Philosophical Ma-
gazine,’ and especially in an independent memoir, published in 1838,
entitled a ‘ Geological Memoir on a part of Western Sussex,’ &c.
The geological structure of the picturesque country around his
residence at Pulborough early attracted Mr. Martin’s attention ; and,
following up the labours of Sedgwick, Fitton, Webster, Mantell,
and Murchison, who had already in great part elucidated the his-
tory of the Upper Secondary Rocks of Sussex, Hampshire, and the
Isle of Wight, Mr. Martin was enabled to throw still more light on
the nature and relations of the Chalk, Firestone, Gault, Shanklin
Sand, and Weald Clay of Western Sussex. In doing this, he gave
greater distinctness to the features of the ‘“ Weald Clay” than had
hitherto been recognized, and he particularly drew attention to the
nature of the valleys and ridges in the Wealden area, considering
the valleys to have been fissures produced by the elevation and
consequent fracture of the strata, and that the drainage-system of
the country follows these lines of fissures to their outlets through
the North and South Downs. These points are treated in detail in
the memoir above alluded to, where also the effects of the de-
rangement of strata in the production of certain valleys (valleys
of elevation, &c.) are largely illustrated, comprising the phenomena
of <“ outliers-by-protrusion,” or ‘inliers”’ as they are now termed
(by the Geological Surveyors); and the contemporaneous or imme-
diately consecutive diluvian action affecting a region so disturbed was
also an important subject of his consideration. The relations of
the London and Hampshire basins, as trough- or basin-shaped con-
tortions of the strata, were a favourite subject with Mr. Martin ;
and observations on the anticlinal line of these basins were pub-
lished from time to time in the ¢ Philosophical Magazine.’ The most
elaborate of this series of ‘ Observations’ was read before the Geo-
logical Society in 1840; but the MS. was mislaid, and not again
found until 1848, three years after which it was published by its
author, with additional matter, in the ‘ Philosophical Magazine.’ It
contains a large amount of information respecting the strata and
lines of elevation and dislocations of the Wealden rocks, and also
on the different zones of drift (gravel, pebbles, and loam) which are
recognizable along the several concentric escarpments in that area,
and which Mr. Martin referred to the diluvial currents consequent
on the upheaval of the Wealden area.

In 1855 Mr. Martin gave the Society a note on his views of the
relations of the gravels of the Sussex coast to the drift of the in-
terior of the Wealden area, stating his belief that they belong to an
outer zone of drift due to one stage of the Wealden elevation, and
probably an early one.

In 1856 he still pursued his favourite researches into the nature
of the diluvial phenomena of the Wealden and of the elevation and
denudation of strata generally, as shown by his papers in the
‘ Philosophical Magazine’ for 1856 and 1857; and, although failing
health began to show itself, his energies were not weakened in this

VOL, XVII, ¢

XXXIV PROCEEDINGS OF THE GEOLOGICAL SOCTETY.

his favourite study. Even in the spring of 1860 he was still en-
gaged with this subject, and but a few days before his decease he
sent a letter on raised beaches to an old friend. .

Joann Frrepricn Lupwie Hausmann, who was elected a Foreign
Member of this Society in 1829, died at Hanover, his native town,
on the 26th of December 1859, in the 78th year of his age. He
had no sooner completed his academical education than he devoted.
himself to the prosecution of geological science. In 1807 he made
a geological tour in Denmark, Norway, and Sweden; in 1809 he
was placed at the head of a Government Mining Establishment in
the then kingdom of Westphalia, and during his administration of
it he established the School of Mines at Clausthal in the Harz
Mountains. On the death, in 1811, of the celebrated Beckmann,
Professor of Technology and Mining in the University of Gottingen,
Hausmann was appointed his successor, with which professorship
was soon afterwards conjomed that of Mineralogy and Geology,
offices which he filled with unremitting zeal and with acknowledged
success until within a few months of his death. During his vaca=
tions, he followed up his geological studies in England, France,
Spain, and Italy. He was the author of a vast number of treatises:
on Mineralogy, Geology, and Technology, and held a distinguished’
place among the scientific men of Germany. On the death of the:
renowned Blumenbach, he was appointed Secretary of the Royal
Academy of Sciences of Géttingen, which he continued to be to the:
time of his death.

It was in the year 1828 that Dr. Fitton, who had been elected
the President of this Society at the preceding Anniversary, first in-
troduced the custom of an address being delivered from the Chair
at our Annual General Meetings. In the then existing circum-
stances of the Society, and for the next fifteen years, when a long
time usually elapsed between the reading of a paper and its publi-
cation in our Transactions, a review of the proceedings of the past
year was interesting and useful. But our Quarterly Journal gives
so full and early* an account of the papers read, that it is now un-
necessary for your President to occupy your time with such a review.
I therefore propose to pass them over, and to bring under your
notice some of the more prominent objects that have occupied the:
attention of geologists in recent times, and which must long con-
tinue to do so, while we endeavour to arrive at a true Theory of
the Earth.

The Geological Survey of the United Kingdom claims, however,
my first attention; for I think that, without beg open to the
charge of arrogance, we may say that it is an offspring of this So-

* A paper by Professor Nicol, which now occupies twenty-nine pages of our
Journal, with fourteen illustrations, was read, referred, printed (the woodcuts

cere) and published between the 5th of December and the Ist of February”
ast. r

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXXV

ciety. The nation is mainly indebted, for the advantages it has’
already and will hereafter derive from that institution, to the genius,
activity, and practical judgment of one of the most accomplished
geologists of the time in which he lived, and for many years a
leading Member in this Society, Sir Henry De la Beche. It has, to
a great extent, the same objects as we ourselves have—the promo-
tion of geology in a strictly scientific point of view,—but with powers
far exceeding any that we possess, in its numerous staff of able men
devoted to the pursuit in all its branches, and with the command of
extensive means supplied by Government. But it has other func-
tions of vast importance, in the development of the mineral treasures
of our country, which, until this Governmunt ScHoon or Minus was
established, was, with few exceptions, leftin the hands of uneducated
persons, the so-called practical men,—a system far from being yet
laid aside, and in strong contrast with that of Germany and France,
countries far less abounding in mineral wealth, where Schools of
Mines have long existed. Such insensibility to the importance of
the culture and encouragement of science on the part of our Govern=
ment and the other Members of the Legislature, in a country like
ours, which has had such ample experience of the benefits derived
from its practical application, can only be accounted for by the
physical and natural sciences haying formed no part of their educa-
tion. The evil effects of this absence of a just appreciation of science
haye of late years been considerably lessened; and there are good
grounds for hoping that they will ere long entirely disappear.

_ My inquiries, at the Museum in Jermyn Street, as to the progress
made by the Survey, and the works connected with it, during the
last year, were most readily responded to by the able and zealous
Director-General, and by all the gentlemen of the establishment,
from whom I sought information. The contributions it has made
to the science of geology, rather than to practical questions, more
especially belong to this address; and most gladly would I have
endeavoured to lay before you some account. of them; but to do so
in any intelligible manner would have led me far beyond the limits
which I must observe in order to notice other subjects to which I
wish to draw your attention. Among the most interesting, how-
ever, | may particularize the work commenced personally by Pro=
fessor Ramsay, and afterwards accomplished, under his superin-
tendence, by his able assistants, Mr. Geikie and Mr. Howell, in the
Lothians. On two sheets of the 1-inch scale Ordnance Map are
delineated the geological features, singularly varied and impressive
in so limited an area, of the Silurian, Devonian, and Carboniferous
strata, with the numerous varieties of felstone, porphyry, and trap,
imbedded and intrusive. No one can examine those maps without
feeling impatient for the publication of the memoirs explanatory of
them, one of which is now in the press. ‘There can be few districts ©
which it would be more interesting to an experienced geologist to.
travel over, or one more advantageous to a learner to explore and
study. I can testify to the great addition to our knowledge, theo-.
retical and practical, which is given by these maps; and I feel

c2

XXXVI PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

assured that my old friend, Mr. Charles Maclaren, who first correctly
pointed out the great geological features of the country round the
Scottish metropolis, will heartily join me in applauding the results
of the recent researches of the Government Surveyors.

When I inform you that during the past year accurate surveys

have been made in England of 832 square miles of Tertiary and
Wealden formations, 40 of Oolitic rocks, 413 of Coal-measures,
Maegnesian Limestone, New Red Sandstone, and Marl,—and in
Scotland, 241: of Coal-measures, Old Red Sandstone, and Silurian
rocks—you will readily believe that a vast mass of facts of the
highest interest to geological science will be brought to light so
soon as the maps, sections, and reports on those surveys are pub-
lished.
' Of information to be derived from publications by the Survey
in the last year, we have five memoirs descriptive of coloured sheets
of the Ordnance 1-inch scale Map of England, previously published ;
four additional coloured sheets of the same map, comprising 1700
square miles ; besides four sheets of the Lancashire Coal-fields on a
scale of 6 inches to a mile; and 53 miles in England, and 48 miles
in Scotland of longitudinal sections, on a scale of 6 inches to the
mile. Other 6-inch-scale maps of the Lancashire and Edinburgh
coal-fields are nearly ready for publication.

To those who can visit the Museum in Jermyn Street, many ad-
ditional opportunities for the careful study of fossils have been
supplied by the labours of Professor Huxley, Mr. Salter, and Mr.
Ktheridge; and a second edition has been published of the very
instructive descriptive catalogue of the rock-specimens, drawn up
by Professor Ramsay, and, under his superintendence, by Messrs.
Bristow, Bauerman, and Geikie.

The information I got at the Mining Record Office, most obligingly
given tome by Mr. Robert Hunt, the keeper, relating to mineral
statistics of various kinds, hardly comes within the range of our
inquiries in this place. One fact I learned which was somewhat
startling, namely, that the drain upon our coal-fields now amounts
to 72 millions of tons per annum. Calculations have recently been
made by Mr. Hull, one of the surveyors, that with an annual drain
of 60 millions of tons, our coal-fields will be exhausted in a thousand
years. Let us hope that our School of Mines will ascertain the
existence of deep-seated beds, such as that in Nottinghamshire,
made known to us by the perseverance, under great discourage-
ments, of his Grace the Duke of Newcastle, to allay our anxiety
for the fate of our remote successors.

You are probably aware that the Geological Survey of Ireland is
placed under the superintendence of a Local Director, assisted by a
staff of District Surveyors, and that there are distinct volumes of
memoirs, with Ordnance Maps, for that part of the United Kingdom,
and a Museum of Practical Geology in Dublin. Mr. Beete Jukes,
the Local Director, has been so obliging as to supply me with full
information respecting their proceedings in the past. year.

The great features of the geology of Ireland have for some time

ANNIVERSARY ADDRESS OF THE PRESIDENT, XXXVI

been known by the map of Sir Richard Griffith—a rare combination
of geological knowledge and persevering industry for one individual
to have produced. But, with few exceptions, and those principally
in the northern part of the island, little had been known of those
minute details of structure which the advanced state of geology
requires. The required closer examination has been for some time,
and is now, in active progress, in conformity with a general plan ema-
nating from the Director-General of the Geological Survey of the
United Kingdom, worked out in its details under the superintend-
ence of Mr. Jukes, of whose eminent fitness for the task, by scientific
acquirements, experience in the field, and untiring energy, you are
well aware,—aided as he is by very competent surveyors.

The Ordnance Map of Ireland, on the scale of 1 inch to a mile, is
divided into 205 squares of equal dimensions; and each square will
be published as a separate sheet. Of those sheets, twenty-seven
geologically coloured have already been published, and twenty-one
are nearly ready. Each sheet (or each small group of sheets, when
it is advisable to unite them) will be accompanied by a printed ex-
planation in 8vo form, containing, first, an account of its physical
geography, showing the form of the ground, the heights of the chief
points, the mean level of its plains, and the levels at which the prin-
cipal rivers enter and leave, that are included in the sheet ; secondly,
a brief general account of the sedimentary formations and eruptive
rocks, with a general sketch of the internal structure ; thirdly, a
sketch of the relation between the form of the ground and its in-
ternal structure; and fourthly, paleontological notes on the most
remarkable fossils. After these come ‘Detailed Descriptions,”
giving an account of the observations made, the places where quarries,
pits, sections, &c. may be seen, and as much of the field-notes as
will guide any one who wishes to examine for himself and verify
the observations of the surveyors, together with notes of the mi-
nerals, mines, drift, and bogs; and woodcut-illustrations are given
with the text. There are, moreover, sheets of longitudinal and
vertical sections, having only the observed data engraved. It is
further intended, when all the sheets are finished, to have condensed
memoirs on large districts.

In these ‘ Explanations’ there is necessarily much repetition ; but
they contain so great an amount of valuable contributions to geo-
logical science in the strict meaning of the term, that, as a general
work, they will well reward an attentive perusal. One of the most
striking features described is the great extent of the surface that is
covered by drift, its vast thickness, and the great height at which it
is found in many places.

Although not connected with the Geological Survey of the United
Kingdom, that now in progress in our Indian Empire is so similar
in its organization, that it is to be reckoned as one of the great
associations through which the sons of Britain are contributing
their share to the advancement of geological science.

It is now ten years since Mr. Oldham, the Superintendent of the
Geological Survey of India, arrived in Calcutta, with the excellent
preparation of haying been Professor of Geology in Trinity College

%XXVill PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

Dublin, and afterwards Local Director of the Geological Survey of
Ireland. But so great were the difficulties with which he had to
contend at the outset, and for a long time afterwards, that. little
more than four years have elapsed since he was able to establish
that regular system of operations by which alone any sure progress
could be made on a truly scientific basis. Before this, to clear the
ground of difficulties and obstacles was the indispensable work.
Although receiving from all in authority much support, the leading
notion of the kind of work for him to do was, to go from place to
place, and, without loss of time, to try to discover coal and other
minerals of economic value, You are probably acquainted with the
first volume of the ‘Memoirs of the Geological Survey of India,’
which appeared in 1859, containing nine treatises—four by Mr. Old-
ham himself, the others by different gentlemen attached to the Survey
—accompanied by numerous maps on a large scale and many illus-
trations. A second yolume has just been issued from the Calcutta
press, containing, a memoir on the northern part of Bundeleund, by
Mr, Henry Medlicott ; a very extensive one on the central portion
of the Nerbudda district, by Mr. Joseph Medlicott ; and one by Mr.
Oldham, “ on the Geological Relations and probable Geological Age
of Rocks in Central India and Bengal.” In a letter which I re-
ceived from him, dated last December, he states—‘‘ You will at
once see that we have been compelled to establish several new
groups to receive (provisionally) the various rocks we have had to
deal with. This has been necessary as well as useful, inasmuch as
for many, and these some of the most widely extended and most
important groups of rocks, we had no definite horizon from which
to work either up or down, Over thousands and tens of thousands
of square miles we have not found a fossil,—some vegetable remains
affording, at the best, imperfect evidence. The richly fossiliferous
rocks of the Himalaya and Sub-himalaya are widely separated from
all the rocks of the peninsula by the broad expanse of the alluvium
which unites the valleys of the Ganges and Indus; and we are
therefore unable to trace out any superposition.”

Mr. Oldham has sent me thirty-five folio plates of the fossil flora
of the Rajmahal Hills, executed in lithography in Calcutta, He
was told that such work could not be executed in India; but he
is not a man to be frightened by difficulties: risking a consider-
able personal outlay for stones, presses, and paper, he persevered,
undaunted by early failures, and succeeded. Another proof of his
energy is the Museum of Practical Geolog ey in Calcutta, and the Geo-
logical Library attached to the Survey. When we consider the vast
range of country over which the survey extends, and the serious ob-
stacles to field-work in such a climate, we cannot too greatly admire
the devoted zeal displayed by Mr. Oldham and the gentlemen who
conduct the surveys under his superintendence. It is to be hoped
that Annual Reports, such as that presented by Mr. Oldham last year,
setting forth the many excellent works which cannot fail to have
the most beneficial influence upon the material prosperity of the
Indian Empire, will secure the zealous and liberal support of its
Government. Let us also hope; for the sake of our science, that a

ANNIVERSARY ADDRESS OF THE PRESIDENT. XXX1X:

field so sure to yield facts of the highest interest will long continue
to be explored by men as worthy of confidence in their ability as
those to whom the great trust is now confided.

The last year has been signalized by the publication of the re-
markable work of Mr. Darwin, ‘On THE Ortern or Species,’ which
has excited no ordinary degree of attention both at home and
abroad. I do not presume to offer any opinion on its merits, be-
cause my previous studies have not been of a kind to qualify me to
be a competent judge. But no one, however unprepared, can fail
to be struck with the truly philosophic modesty and candour of the
author. His acute and well-stored mind had been directed to the
subject for more than twenty years, during which time he accumu-
lated a vast mass of facts, and had carried on numerous ingenious
experiments. These he has exhibited in detail before his readers,
and has calmly stated the conclusions to which they have appeared
to him to lead; and so far from stating those conclusions in any
spirit approaching to dogmatism, he has seen and even imagined the
objections which, as he himself says, might be justly urged against
his theory ; and in his replies he shows no desire for victory, unless
won by the arms of sound reasoning. It has been observed by a
critic of no ordinary power, by one eminently qualified to sit in
judgment on such a work, that “all competent naturalists and
physiologists, whatever their opinions as to the ultimate fate of the
doctrines put forth, acknowledge that the work in which they are
embodied is a solid contribution to knowledge, and inaugurates a
new epoch in Natural History.” The writer adds, “ our object has
been, in this eriticism, to give an intelligible account of the esta-
blished facts connected with species, and of the relation of the expla-
nation of these facts offered by Mr. Darwin to the theoretical views
held by his predecessors and his contemporaries, and, above all, to
the requirements of scientific logic. We have ventured to point out
that it does not as yet satisfy all these requirements ; but we do not
hesitate to assert that it is as superior to any preceding or contem-
porary hypothesis in the extent of observation and experimental
basis on which it rests, in its rigorously scientific method, and in
its power of explaining biological phenomena, as was the hypothesis
of Copernicus to the speculations of Ptolemy. We should leave a
very Wrong impression on the reader’s mind if we permitted him to
suppose that the value of this work depends wholly on the justifica-
tion of the theoretical views which it contains. On the contrary,
if they were disproved tomorrow, the book would still be the best
of its kind, the most compendious statement of well-sifted facts
bearing on the doctrine of species that has ever appeared.” If
common report and intrinsic evidence are to be relied upon, the
author of the above criticism is no less a person than our distin-
guished Secretary, Professor Huxley.

There are two chapters, however, in the work, upon which I
venture to offer this opinion, that it becomes almost a duty of the
President of this Society, on an occasion like the present, to recom-

xl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

mend to the careful study of geologists. I refer to Chapter IX., “ On
the Imperfection of the Geological Record,’ and to the following
chapter, ‘‘ On the Geological Succession of Organic Beings.” They
will do well to study with great attention their valuable contents.
They will there be taught a most useful lesson of the caution to be
exercised in drawing conclusions from organic remains which may
involve the grave questions of the age and correlation of formations ;
and when disposed to name an imagined new species, they will be
reminded that “naturalists have no golden rule by which to di-
stinguish species and varieties,’ and they will learn to pause until
they feel assured that no sources of mistake have been overlooked,

It would be both useful and interesting if the annual Presidential
Address were to contain a summary of the most prominent geological
memoirs contained in the Transactions and Journals of foreign
countries; but the field over which the researches in geology now
extend is so vast, that it is beyond the power of any individual to
give even a brief sketch of the labours, in a single year, of its more
eminent foreign cultivators. Were the limits within which an ad-
dress of this kind ought to be confined in itself no obstacle, there is
the manifest impossibility for any one individual to possess that ac-
quaintance with what has been done in the past year in chemistry,
mineralogy, physics, botany, and zoology, which would enable him
to touch upon even the salient points in those branches which bear
upon our science; and, as you are aware, geology lays every one
of them under contribution. But although a review of our own
proceedings be unnecessary, and asummary of the labours of foreign
cultivators of natural science be impracticable, our annual meetings
are fit occasions for calling the attention of our Fellows to some of
the more important subjects which have more recently occupied the
attention of geologists. Among those, the researches in what may
appropriately be called Chemical Geology occupy a prominent place.

The application of chemistry to the explanation of geological phe-
nomena has hitherto received more attention on the continent than
with us. The greater features of the earth’s structure and palzon-
tology in its various branches have, with few exceptions, been the
ehief study of British geologists. When organic remains no longer
present themselves in the older formations, or are nearly obliterated
in the newer, the term metamorphic has become very current; but
the origin of metamorphism (that is, the exciting causes of the mole-
cular actions by which it could have been brought about in accord-
ance with known chemical laws) has rarely been a subject of in-
vestigation with us. Metamorphism must, in every case, be the
result of chemical action ; and we can only arrive at a just concep-
tion of the processes by which the various forms under which it
presents itself could have been produced, by illustrations afforded by
experiments in the laboratory, under the guidance of an accurate
acquaintance with chemical agencies and the laws of combination
among mineral elements. So also it is only by the same safe
guidance that we can hope to arrive at a right knowledge of the

ANNIVERSARY ADDRESS OF THE PRESIDENT. xli

nature of the eruptive rocks, of the changes which nearly all the
stratified rocks, of all ages, have more or less undergone since their
constituent detrital parts were first’ deposited, whereby loose mud
and sand have been converted into hard and often crystalline rocks,
of the formation of the accessory simple minerals which many of the
strata include, and of the complex phenomena of mineral veins. In
the whole range of paleontology even, there is scarcely a single
organism that exists in its pristine state; neither shell, bone, nor
plant remains in the condition it was when first entombed. The
great problem, by what process vegetable matter has been converted
into bituminous coal, is still unsolved. Not only in early times, but
even at no distant period, it has not been uncommon for geologists
to build up theories by invoking the aid of chemical solutions and
vapours, without even an attempt to show that such agencies were
even possible. It will doubtless be ever impossible for us to subject
substances to operations in our laboratories more than resembling in
kind those which we suppose them to have undergone in the interior
of the earth, in order to produce metamorphism, or to form eruptive
rocks and mineral ves ; we can never know the effect of processes
continuing under enormous pressure for thousands of years ; but we
may obtain results, on a small scale, so closely resembling, indeed
often identical in composition and form, natural productions, as to
entitle us to infer that the processes of nature have been analogous
to those which we have employed.

The celebrated experiments of Sir James Hall, more than half a
century ago, on the effects of heat modified by compression, may be
said to have formed an epoch in the history of theories of the earth.
They were undertaken for the purpose of testing the soundness of
the theory advanced by Hutton, that rocks, including limestone, had
been consolidated by the effect of heat under powerful compression,
which he had been accustomed to discuss with that illustrious philo-
sopher. Hall, then a young man, was not convinced by the argu-
ments of his master in geology, and especially as they applied to
carbonate of lime, a substance, which, as he said, every limekiln
showed to be changed in its nature by heat. But fearing that the
results of the experiments he was contemplating would not confirm
the bold hypothesis, from tenderness for the then declining health of
the amiable old man, he postponed them until after his death in
1797. He was patient in his researches ; for they were carried on
for several years, and amounted, as he states, to the large number
of 156. He was no less cautious in drawing his conclusions ; for,
although the results he was obtaining were known to Playfair and
his other geological friends, he first made them known to the public
by his memoir read before the Royal Society of Edinburgh on the
5th of June, 1805. His experiments, though varied in form, were
similar in kind. He subjected finely pulverized common limestone,
sometimes pulverized calcareous spar, enclosed in gun-barrels or in
tubes bored in masses of wrought-iron, firmly pressed down and
hermetically sealed, in a furnace to an intense heat. With regard.
to the pressure, Sir James Hall states that he tried various amounts :

xhi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

52 atmospheres, equal to 1700 feet of sea; 86, answering to nearly
3000 feet ; and 173, to 5700 feet of sea—that is, a little more
than a mile. The results were, that under the first of these pres-
sures the powder was changed into a compact limestone, under
the second to a marble, and under the last it underwent complete
fusion, and acted powerfully on other rocks. He states that on ex-
hibiting a specimen of the saccharoid marble to the workman he
employed to polish it, the man observed that, if it were a little
whiter, the quarry from which it had been taken would be of great
value.

The soundness of the conclusions to which Hall arrived has been
lately called in question by Dr. Gustav Rose, Professor of Geology
in the University of Berlin, in a memoir published in the ‘ Monats-
bericht’ of the Berlin Academy for July last, giving an account of
two experiments on the effect of a powerful heat on earthy lime-
stone enclosed in a gun-barrel hermetically sealed,—-experiments so
far analogous to some of those of Sir James Hall. The barrel was
placed in a newly erected gas-furnace, in which the heat was suffi-
ciently great to melt easily large masses of platina. He describes
the changes which the earthy limestone was found to have under-
gone, and thus concludes:—‘ From these experiments it would
appear that chalk and compact limestone, when subjected to a high
temperature in a closed space, are not changed into distinct crystalline
spar, and that, as a general fact, rhomboidal carbonate of lime is not
formed by the so-called dry process. When the descriptions of Hall’s
experiments, as well as those which Bucholz afterwards made with
the same object, are examined, it appears extremely probable that
the results were what the authors describe, but that they mistook the
hard-baked but unaltered chalk for crystalline marble. Although
those experiments of Hall have been so much quoted, as affording
an explanation of geological phenomena, and in support of theoretical
views, they have not received any confirmation from having been
repeated by others ; and the experiments of the present author show
how hasty the general conclusions were which were drawn from
them.”

With every respect for my friend the Professor, | think that I
may turn round upon him and say that he has been somewhat hasty
in considering that his experiments prove that mistakes were made
by Hall in his descriptions of the results of his numerous experiments,
all agreeing while obtained in so many different ways; for the Pro-
fessor states that in both of his experiments the gun-barrel burst
(atwhat stage of the experiment, he does not say); and thus one of the
essential conditions in Hall’s experiments was wanting, viz. continued
great pressure. I consider therefore that these experiments of Pro-
fessor Rose in no degree invalidate those of Hall, so long considered
to support, in no inconsiderable degree, the hypothesis of Hutton.

In 1816 Professor Hausmann of Gottingen drew attention to the
explanation of geological phenomena by observations on some products
obtained from smelting-furnaces. Among the most remarkable re-
sults of the condensation of the vapours of smelting-furnaces is the

ANNIVERSARY ADDRESS OF THE PRESIDENT. - xii

formation of crystals of felspar, which have been frequently found in
the copper-works of Mansfeld—the more remarkable as all attempts
to obtain them by direct fusion have hitherto failed. The first direct
‘synthetic experiments to obtain minerals artificially by igneous
fusion were made successfully by Berthier, followed in 1823 by
Mitscherlich. They obtained many crystallized simple minerals
identical with those of nature. These researches for a long time led
to the belief that fluidity by heat could alone have yielded such
results ; but within the last few years, and especially within a short
time, other researches have produced a conviction that water, com-
bined with heat and pressure, must have acted a very important
part in most of the operations ascribed to the action of heat and
pressure only, from the earliest periods of geological time.

That an enormous pressure must take effect, even at moderate
depths, is self-evident ; and that a very high temperature prevails in
the interior of the earth is proved by the existence of volcanos in all
parts of the earth, which from time to time pour forth streams of
molten incandescent rock; and that a heat sufficient to keep rocks
in a fused or viscid state has existed from the earliest geological time
is made manifest by the veins and intruding masses of granite and
the other eruptive rocks that penetrate all formations, from the
oldest to the newest strata; for the cone of trap that traverses the
Carboniferous rock and rises to the summit of Arthur’s Seat, Edin-
burgh, is now believed to be of tertiary age. That this internal
heat is permanent is further demonstrated by the increase of tem-
perature as we descend from a short distance below the surface, in
all parts of the earth where the experiment has been made. We
have thus undoubted proof of the existence of two of the three great
active agents in the laboratory of nature, heat and pressure.

Without assuming the existence of great internal supplies of
water or its elements, there can be no doubt that it must exist in
the interior of the earth to a vast extent. The amount of that
which is carried off by rivers must bear a small proportion to that
which, falling from the atmosphere upon the wide-extended surface
of the land, must be carried to great depths through porous rocks,
and by the innumerable cracks and fissures by which every rock is
more or less traversed. The existence of subterranean rivers and
of accumulations of water at great depths is proved by artesian
wells; and, as we know no limits to the downward extent of faults
and fissures, there is every probability that much of the water that
falls on the surface must penetrate to depths where a high tem-
perature exists ; as is shown by hot springs, the temperature of which
we know to have continued undiminished for centuries, and by the
enormous volumes of watery vapour poured forth by volcanos. It
probably reaches depths where the heat will bring it not only to the
boiling-point, but, under great pressure, to a far higher temperature.
According to the researches of Mr. Robert Hunt, the rate of increase
of temperature, from about 100 feet below the surface, is 1° of Fahr.
for every 50 feet in penetrating through the first 100 fathoms; 1°
for every 70 feet in the next 100 fathoms; but when the depth ex-

xliv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

ceeds 200 fathoms, the increase is only 1° for every 85 feet of
depth*, Supposing the increase for greater depths to be at the
average rate of 1° for every 100 feet, the temperature of the melting-
point of cast-iron, viz. 2786° of Fahr. T, Will exist at a depth of
somewhat less than 443 miles, that is th of the earth’s equatorial
radius. A cubic inch of water at 212° expands to nearly a cubic
foot of steam, or, more accurately, to 1696 times its volume. By an
addition of the pressure of one atmosphere, the mercury standing at
30 inches, the boiling-point is raised from 212° to 249°; and by con-
tinuing the heat, without allowing the steam to escape, the boiling-
point rises still higher ; and the elasticity of the steam increases with
increasing rapidity as the temperature rises. By the experiments
of Regnault, it has been shown that by a pressure of

2 atmospheres, the boiling-point is 249-5
3

” ” ” 273°3

4 ” > ” 291-2
By Fi ged oad cee
10 ” ” ” 356°6
20 ” ” ” 415-4

As the temperature rises by equal additions of heat, the increase of
elasticity 1s more rapid at high than at low temperatures, But it is
only when in contact with a body of water from which fresh steam
is constantly rising that the elasticity augments in this manner, and
thus produces a force sufficient to rend asunder the strongest vessels.
If dry steam alone be heated, it follows the law which regulates the
expansion and elasticity of gaseous bodies in general?. Thus, in-
dependently of the action of water as a constituent of mineral sub-
stances, we may, with every degree of probability, consider high-
pressure steam to have been the power which rent, shattered, and
elevated the sedimentary strata in all geological periods, which
drove the softer granites and trappean rocks into rents, and protruded
them to the surface, producing the jagged fractures of the upheayed.
strata—that evident snapping of a hard substance, leaving splintered
ends and edges. ‘In the Alps of Switzerland and Savoy, we find the
most stupendous monuments of mechanical violence, by which strata
thousands of feet thick have been bent, folded, and overturned,
marine secondary formations upheaved to the height of 12,000, and
some eocene strata to 10,000 feet above the level of the sea§.” To
what more probable agency than that of high-pressure steam can we
ascribe such effects ?

The powerful part which water has played in the formation of
minerals and rocks is shown in a very clear manner by Professor
Gustav Bischof of Bonn, in his elaborate ‘ Lehrbuch der Chemischen
und Physikalischen Geologie,’ in four 8vyo volumes, the first published
in 1847, the last in 1855, showing a vast amount of indomitable

* Sorby, Quarterly Journal of Geological piety vol. xiv. p. 495.
+ Miller’s Chemistry, vol. i. p. 194. Ib, yol. i. p. 250.
§ Lyell, Manual of Geology, dth ed., p. 621.

ANNIVERSARY ADDRESS OF THE PRESIDENT. xlv

perseverance in laborious research so peculiarly characteristic of his
countrymen. His recorded experiments extend over a period of
more than thirty years. His ‘ Lehrbuch,’ even in the English trans-
lation in a condensed form (executed with the cooperation of the
author, under the auspices of the Cavendish Society), does not appear
to have received from the geologists of this country a due attention,
while he is constantly referred to as a high authority by the most
eminent geologists of France and Germany.

The agency of water in the formation of minerals was shown nearly
forty years ago by Becquerel, who succeeded in obtaining by a humid
process galena, sulphuret of antimony, and other minerals occurring
in veins. M. Scheerer*, in an elaborate memoir on the plutonic
nature of granite, in 1846, on a review of the chemical and mechanical
constitution of that rock, and of the many accessory minerals it often
contains, and especially their different degrees of fusibility and the
different temperatures at which they crystallize, arrived at the con-
clusion that the various phenomena they exhibit, as simple minerals
and in combination as a rock, can only be explained by the com-
bined action of heat and water. He tells us that he began to study
the granitic rocks of Norway in 1833, fully impressed with a belief
in the plutonic (that is, the solely igneous) origin of granite, but
that the result of a most careful research was an entire overthrow
of his early creed, and that ‘Vidée la plus juste que l’on peut se
former sur l’origine de ces roches est celle qui attribuerait aux deux
éléments, 4 l’eau et au feu, une égale puissance créatrice.” M. Elie
de Beaumont, in 1847, in his very instructive essay “Sur les éma-
nations volcaniques et métalliferes,” brings forward numerous in-
stances which appear to him to prove the existence of water in the
constitution of eruptive rocks and mineral veins. Thus, while the
igneous fusion of granite is, in his opinion, proved beyond all doubt
by many phenomena that accompany it, he considers it to be no
less capable of proof that water must have entered into its compo-
sition while in that state. He observes that M. Scheerer of Chris-
tiania has given many reasons why granite in fusion must have
contained water, that it was in combination with it at the time of
its eruption, and that it was retained until after the final cooling of
the granite; for many simple minerals containing water as a con-
stituent are found in that rock. M. de Beaumont conceives that
there is, in truth, no reason against believing that granite contained
water at the time of its eruption; for the lavas of existing volcanos,
at the time of their ejection, contain a large amount of water,
which in part separates in the form of vapour, but is not entirely
dissipated for many yearst. In treating of different kinds of

* Bulletin de la Soc. Géol. de France, 2de série, vol. iv. p. 468.

t “ Dans les exhalaisons volcaniques, il est un corps qui n’a pas tout d’abord
fixé l’attention, parce que, sous l’empire des idées anciennes, il semblait tout a
fait inerte, surtout en présence des minéraux dont il s’agit d’expliquer la forma-
tion, mais auquel pourtant le premier réle parait devoir étre dévolu, dans les
phénoménes métamorphiques aussi bien que dans les éruptions des volcans: ce

corps c’est l’eau, qui se trouve dans ces exhalaisons, non en quantité minime,
comme les yapeurs, mais, au contraire, comme le produit 4 la fois le plus abondant

xlvi PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

quartz, he states that it is probable that water has played a part

in the formation of all of them*.

The powerful action of water at a high temperature, under great

pressure, upon mineral substances has been recently most satis-

factorily proved by the synthetic experiments of M. Daubrée}. In ©

stating the object of his researches, he observes—‘‘ No one is un-
acquainted with the results obtained long ago by Berthier and
Mitscherlich, and more recently by Ebelmen, regarding the forma-
tion of silicates at high temperatures by means of fusion. Thus,
while the dry process yielded by various methods crystallized anhy-

drous silicates, some of which are identical with those found in”

metamorphic rocks, it had hitherto been found impossible to obtain
similar imitations by the humid process. Synthetie experiments,
guided by geological induction, couldalone solve the question. Such
is the aim of those in which I have endeavoured to bring into play
affinities capable of producing like combinations.” He enclosed the

minerals he operated upon in a glass tube partially filled with water,

which he inserted in a strong iron tube, between which and the glass
tube water was poured, to counterbalance the tension of the vapour
in the glass tube, which would have caused it to burst. The iron
tube being firmly closed by a screw, was placed in a bed of charcoal
powder, and exposed for several weeks to the heat of a gas-making
furnace, in which the heat could not be less than 850° Fahr., and
when taken out was allowed to cool gradually. With all the precau-
tions he could take, so great was the tension of the vapour, that, of
the many experiments, two tubes out of three exploded.

After being exposed to the heat of the furnace for a week, the
structure of the glass was no longer recognizable. It was entirely
changed into a white substance, perfectly opake, and adhering to the
tongue, exactly resembling kaolin. In some of the experiments the
form of the tube was preserved, but in others the glass was reduced
to a white powder. Entirely new combinations had been formed :
the water had become highly charged with an alkaline silicate; and
the opake substance, which at first sight had appeared amorphous, was
found to be entirely composed of crystalline elements. They were
seen, even without the aid of a magnifying glass, to consist of limpid
colourless crystals, haying the ordinary bipyramidal form of quartz
and its usual appearance; they were, in fact, no other than crystallized

et plus constant des éruptions, dans toutes les régions du globe. La singulieére
propriété que possedent les silicates incandescents des laves de retenir pendant
fort longtemps, et jusqu’au moment de leur solidification, des quantités d’eau
considérables, démontre clairement que l’action de Ja chaleur n’exclut pas celle de
Yeau, et parait annoncer que cette derniére a, méme a ces hautes températures,
une certaine affinité pour les silicates. Nous ne connaissons des masses situées &
une certaine profondeur dans notre globe que ce qu’en apportent les volcans: or
ces déjections renferment toutes, sans exception, de l’eau, soit combinée, soit
mélangée; nous sommes done en droit de penser que l’eau joue un role tout 4
fait important dans les principaux phénoménes qui émanent des profondeurs.”—
Daubrée, Etudes et Expériences Synthétiques sur le Métamorphisme, p. 85.
* Bulletin de la Société Géologique de France, 2de série, vol. iv. p. 1249.

+ Observations sur le métamorphisme, et recherches expérimentales sur quelques:

uns des agents qui ont pu le produire.

ANNIVERSARY ADDRESS OF THE PRESIDENT. “xivii

silica. Some crystals formed in this way, at the end of a month,
attained the size of two millimetres (=-07874 inch). They were
often insulated in an opake paste, sometimes adhering to the sides
of the tube, forming true geodes, impossible to distinguish, except im
size, from those which crystalline schists often contain. The white
substance which forms the greater part of the residue of the trans-
formation of the glass is not amorphous, but forms acicular crystals
which cannot be better compared than to the dust of fibrous horn-
blende passing into asbestus. They proved on analysis to be com-
posed of constituents nearly identical with wollastonite. M. Daubrée
adds, ‘It is impossible to look without astonishment upon so com-
plete a change in the physical and chemical condition of glass obtained
by a very small quantity of water, in weight not exceeding one-half
of that of the glass so transformed.” Under the same conditions,
moreover, water exerts an influence on crystallization of the most
remarkable kind on quartz and the silicates. At a temperature of
about 850° it dissolved the elements that had been combined in the
glass by a much more powerful heat, but without its intervention.
Its vapour, under the conditions of the experiments, by reason of its
acquired temperature and density, acts chemically like water in the
fluid state. ;

In the presidential address of my predecessor, Professor Phillips,
in 1859, mention is made of the observations of M. Daubrée, of
Strasbourg, on the hot springs of Plombi¢res, then recently made
known; and I now recur to them in greater detail because of their
important bearing on the subject to which I am now endeavouring
to call your earnest attention, namely, the increasing conviction on
the minds of geologists, produced by experiments in the laboratory,
that water must have played a most important part in the origin of
simple minerals, of the eruptive rocks, and in metamorphic action.
M. Daubrée made the experiments above described with the water
of those springs concentrated to a twentieth of its volume, and he
also made a careful examination of their effects upon the mineral
substances over which they flow. They rise on the south-west flank
of the Vosges Mountains, and issue from a porphyritic granite,—the
temperature of the hottest bemg 78° C. (=1723° F.), and others
from 15° to 30° C. (=59° to 86° F.). They contain only a minute
quantity of saline matter, not more than half a grain to the quart ;
but silicate of potash predominates. The Romans had formed in
it a thick mass of concrete, with channels or gutters, to convey the
water to the baths which they constructed in that place, and which
still exist. It is composed partly of bricks and partly of the neigh-
bouring bunter-sandstein, united by a mortar of lime without sand.
This concrete is about 10 feet thick ; and M. Daubrée found that the
water has filtered through the crevices of the mortar in a continuous’
stream. The calcareous cement and even the bricks themselves have
been partially metamorphosed. The new combinations produced are
found especially in the cavities of the mass, where they form mam-
millary concretions, sometimes crystallized. The most remarkable
of these in point of number are silicates of the zeolite family, and:

xlviii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

particularly apophyllite and chabasie*. Besides these, there are
some other zeolites, together with opal, mammillary hyalite (per-
fectly transparent and undistinguishable from the hyalite of basalts),
aragonite, and calcareous spar. The apophyllite is found only in
the cavities of the mortar; it is asilicate containing lime and potash ;
whereas the chabasie, a double silicate of alumina and potash, occurs
exclusively in cavities of the brick. The neighbouring granite has
never been found to contain any zeolites ; but the water contains the
elements of that family of minerals, potash and lime, the former
being derived from the decomposition of the felspar of the granite,
the latter from the mortar. Thus it appears that minerals which
we find in veins and in eruptive rocks may be formed by the joint
agency of water and heat, although that heat may not exceed 158° F.
In prosecuting these experiments, M. Daubrée obtained well-formed
crystals of the transparent variety of augite, called diopside. Fir-
wood was changed into a black compact shining body, having all
the appearance of pure anthracite, and so hard as to be scratched
with difficulty by a steel point. It closely resembles the anthracite
that accompanies veins of silver in gneiss at Kongsberg in Norway.

I have said that the experiments of Sir James Hall formed an
epoch in the history of theories of the earth. In the same light, but
in a still higher degree, the observations and synthetic experiments
of M. Daubrée, showing the powerful and widely extended agency
of water, will probably be viewed as an epoch in our science. He
has demonstrated that water, accompanied by heat and compression,
with a very minute quantity of potash, has a solvent power upon a
wide range of mineral substances, especially upon silica, the earth
of all others the most prevalent in the structure of the globe. He
has further proved that the degree of heat imagined to be necessary
for the production of certain minerals has been much exaggerated,
and that products characteristic of metallic veins and volcanic rocks
may be formed at a temperature not exceeding 158° F. He refers
especially to the zeolite family so constantly found in trappean and
volcanic rocks, both as a constituent part, and as filling vesicles,
and which, therefore, may have been formed when the process of
cooling had been far advanced. He reminds us that zeolites have
been found in the fragments of tertiary limestone that occur in the
basaltic tuff of the Puy de la Piquette in Auvergne. He has further
shown that the molecular state of the water in lavas, be it what it
may, has had a great effect in the formation of silicates, even when
anhydrous. It causes them to separate, and to crystallize at a tem-
perature much below their point of fusion ; it enables them to cry-
stallize in an order of succession different from that of their fusibility:
thus, for example, leucite, an infusible silicate of alumina and potash,
occurs in lavas in well-formed crystals, often of large size. To this,
Ludwig, in his German translation of Daubrée’s essay, adds that the
crystals of leucite often contain fragments of lava, and even small

* In sixteen different species of zeolite, water has been found to enter largely

into the composition of each, varying from 8 per cent. in some specimens of
analcime, to nearly 22 per cent. in some specimens of chabasie.

ANNIVERSARY ADDRESS OF THE PRESIDENT, xlix

erystals of the very fusible mineral augite. There is an important
remark of Daubrée, that, at high temperatures, so small a quantity
of water is sufficient to produce crystallization of silicates, that that
existing in clays, or even that mechanically contained in rocks, com-
monly termed the water of the quarry (eau de carriére), appears to
be all that is required to develope, when assisted by heat, very
energetic action,

Metamorphism.

The term “ metamorphic ” was first given by Sir Charles Lyell in
1833, as a designation for certain of the older strata considered to
have been altered by subterranean heat. He states, in the last
edition of his ‘Manual of Geology,’ that by metamorphism he means
an action, existing in the interior of the earth at an unknown depth,
whether thermal, hydrothermal, electrical, or other, analogous to that
exerted near intruding masses of granite, which has, in the course of
vast and indefinite periods, and, when rising perhaps from a large
heated surface, reduced strata thousands of yards thick to a state
of semifusion, so that on cooling they have become crystalline like
gneiss. He enumerates as the principal metamorphic rocks—gneiss,
mica-schist, hornblende-schist, clay-slate, chlorite-slate, hypogene-
limestone, and certain kinds of quartzite. These rocks, he says,
When in their most characteristic and normal state, are wholly
devoid of organic remains, and contain no distinct fragments of
other rocks, whether rounded or angular, and that, however cry-
stalline they may become in certain regions, they never, like granite
or trap, send veins into contiguous formations, whether into an older
schist or granite, or into a set of newer fossiliferous strata. Here
then we have the term distinctly conjoined with a theory of the
agency by which the metamorphism is produced, and an equally di-
stinct restriction of the term to particular rocks.

But such a restriction is now disregarded both in this country and
elsewhere, and the term metamorphic is applied to any sedimentary
rock, secondary or tertiary, which is altered from its original state
to a hardened or crystalline structure, without reference to any
theory of the agency by which the change was produced, however
diversified the nature of the rock may be. Thus, M. Coquand, in his
‘Traité des Roches,’ published in 1857, has a whole family of Roches
métamorphiques, comprising thirteen species and no less than eighty-
eight varieties, as follows :—

Mica-schiste, embracing... 11 varieties. | Gypse, embracing ......... 7 varieties,
Tale-schiste 4 sco J) Ms | clrodonyabetis 5 copeaoae DE
Chlorite-schiste ,, PD) 3 | Alaunite Pa Us udnaicesaiats Daly as
Amphibolite-schiste ,, ... 5 - | Quartzite PW ehee ct Raa Laid: BS
Argiloschiste _,, Brawls) u Jaspe Benn races couche iene,
Caleaire 7 eal 2, a Porcellanite ,, ..s...+06 Ose

Dolomie % ro NU
Taken in its widest sense, the term might be applied to every altered
rock, be its age what it may ; for a structural change is as distinct
in many sandstones and limestones as in the older strata, Studer
VOL, XVII. d

] PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

and Merian found in the Alps of Glarus the flysch passing into
rocks as crystalline as the mica-schist and gneiss of St. Gothard and
Chamouny; and Sir R. Murchison has shown that large portions
of the flysch in the Grisons have been converted into a crystalline
rock, and that in many places in the Alps, secondary and even tertiary
limestones are changed into saccharoid marble undistinguishable from
that which has been called primary.

But it is obvious that the metamorphism of materials so very
different in their nature cannot have been brought about except by
very different chemical operations, and that it could not have been
produced in all by the materials having been exposed to a deep-seated
internal heat; for the altered rocks alternate with others of vast
thickness which have undergone no change, and through which the
heat could not have been transmitted. It is nevertheless yery
doubtful whether the term is ever applied without some vague, in-
distinct belief that internal heat has been the great agent in the
change ; this certainly is not a very philosophical state of mind, and
shows how much it behoyes us to be cautious in the use of a term
involying theory unsupported by experimental proof, To the fact of
the change of structure we cannot shut our eyes; it is plain and
palpable; and we must give ita name; but the name should be free
from any unproved theoretical import. No true theory of the earth
can be arrived at until the theory of metamorphism, in its various
phases, has been established on sound chemical principles by synthetic
experiments.

I have already referred to the memoir of M. Daubrée on Meta-
morphism, published in 1858. In the same year there appeared the
‘Etudes sur la Métamorphisme’ of M. Delesse. He truly observes,
at the very outset of his work, that “‘metamorphism comprehends
phenomena which are extremely complex, and which are for the
most part involved in great obscurity.” He considers that the subject
is divisible into two distinct forms,—the one being normal or general
metamorphism, the result of causes most frequently invisible, and
which have operated on a great scale ; the other abnormal, or rather
special, metamorphism, the result of accidental causes, the effects of
which are of limited extent. It is to this last form, which he also
designates ‘‘ metamorphism of contact,” that this publication is con-
fined. But there can be no doubt that normal or general metamor-
phism is by much the most important subject for our careful study :
that of contact is only a subordinate branch of the great question,
Researches and experiments relative to it are doubtless of great value
as indications of the causes of the greater operation, and as likely to
lead to some well-founded theory of the many phenomena of general
metamorphism. But the processes, whatever they were, must have
been very different which caused the alterations produced, on many
occasions, when an eruptive and a stratified rock came in contact,
and that transformation which has extended over thousands of
square miles. In the former case the rock affected and that affect-
ing are before us, and the change was probably the work of a com-
paratively short time; while in the latter case all is hidden, and the

ANNIVERSARY ADDRESS OF THE PRESIDENT. li

operation was, with greater probability, the slow continuous effect of
thousands of years of chemical action under enormous pressure.

M. Delesse has very recently presented us with another work in
which the larger subject is treated of with great minuteness of detail,
and in which he has brought to bear his extensive observations, his
mineralogical knowledge, and his skill and experience in chemical
analysis. He has been so obliging as to send me an unpublished
copy of his memoir, which, consisting of 90 quarto pages, will form
a part of a forthcoming volume of the ‘ Mémoires de l'Institut de
France.’ In this work he by no means confines the term metamor-
phism to those rocks to which it was originally applied by Lyell,
and to which it is restricted by many geologists, but gives it a very
wide range. He says at the very outset, ‘‘ Toutes les roches qui
entrent dans la composition de l’écorce terrestre ont pu étre modifiées
par le métamorphisme général” (p. 129); that ‘il est bien con-
staté maintenant que les roches métamorphiques se sont formeés a
toutes les époques géologiques”’ (p. 152). He speaks of ‘ roches
métamorphiques appartenant a tous les terrains, depuis le silurien
jusquw’au nummulitique” (p. 155). He considers that the for-
mation of coal in all its varieties, from lignite to anthracite, is the
result of general metamorphism: “ Le métamorphisme général subi
par les combustibles est identique 4 celui qui est éprouvé au contact
de roches non-volcaniques” (p. 160). It is evident, therefore, that
metamorphic action, in the sense in which it is used by M. Delesse
in this memoir, becomes nothing more than a general term for that
agency or variety of agencies by which mineral substances have un-
dergone alterations from their original state throughout all geological
periods, and is the abandonment of a very convenient technical desig-
nation for a particular class of rocks—those inferior basic rocks which
have been held to have been for the most part transformed from a
prior condition of sedimentary deposits.

On the 30th of last June, the Academy of Sciences of Paris awarded
to M. Daubrée the Bordin Prize for an essay entitled ‘Etudes et
Expériences synthétiques sur le Métamorphisme et sur la formation
des roches cristallines,” which has since been published. He com-
mences with the following remarks :—‘“ One of the most important
questions which geology is called upon to solve, is to settle the parts
in the formation of the solid envelopment of the globe which are to
be ascribed respectively to aqueous and igneous action. Although it
has been long debated, it has as yet received no definite solution ; it
has even become complicated, since by a more rigorous examination
of different rocks we have discovered evidence of a twofold origin.
Was it at the very moment of their formation that these ambiguous
rocks received this double character, or was the one consecutive on
the other ? and, in the latter case, how can we account for such a
succession of effects? These are subjects the study of which con-
stitutes what in their more extended and general sense we term
metamorphism.” He gives a historical sketch of the gradual de-
velopment of those observations on the structure of rocks by some of
his predecessors which have led the way to the views now generally

d 2

li PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

adopted. In giving a list of the English geologists who have ad-
vanced this branch of our science, he most strangely omits the name
of Lyell—of him who was the first, twenty-seven years ago, to suggest
this modification and restriction of the Huttonian theory, and who
in the several editions of his ‘ Manual of Geology,’ a work quoted by
M. Daubrée, has so fully discussed the whole question of metamor-
phism, so far as it had advanced, not even omitting the possible
agency of water at an intensely high temperature, in producing it,
by an internal movement and re-arrangement of the molecules*.
After noticing some remarkable statements in the works of Des-
cartes and Leibnitz, he passes to the more modern names of Buffon,
Saussure, Pallas, and Werner, and then dwells at some length on
Hutton and his illustrator Playfair, in whose works, he says, we
find established and developed, for the first time, certain fundamental
principles of modern geology, and especially metamorphism. After
pointing out the fundamental hypothesis of Hutton, that the strata
had been formed by the detritus of pre-existent rocks and afterwards
consolidated by heat, he adds,“ Thus, by an idea entirely new, the
illustrious Scotch philosopher showed the successive cooperation of
water and the internal heat of the globe in the formation of the same
rocks. It is the mark of genius to unite in one common origin phe-
nomena very different in their nature. Hutton first pointed out that
subterranean heat had not only consolidated and mineralized the
deposits at the bottom of the sea, but had moreover raised up and
thrown into inclined positions beds which had originally been hori-
zontal. Another discovery due to Hutton, which has also been of
capital importance in geology, is the eruptive origin of granite. He
further demonstrated, by numerous examples exhibited in Scotland,
that the trap-rocks had been injected into regions where there is no
indication of a yoleano. Hutton explains the history of the globe
with as much simplicity as grandeur. Although, by considering the
process of decay and renovation a continuous phenomenon, he has
thrown a shade over his noble conception, he has rendered immense
services in demonstrating that natural causes which operate under
our view are sufficient to explain the history of the globe, and that
it is unnecessary to have recourse to other modes of action than
those exhibited by nature in our own day; whereas other systems
that had been devised assumed, on the contrary, events which had
no analogy with what we now witness. Thus Hutton is truly the
founder of the fertile principle of the transformation of the sedimentary
rocks, by the action of heat. Nevertheless, we shall notice hereafter
that there are many deductions to be made from conclusions so
absolute. Like most men of genius who have opened up new paths,
Hutton exaggerated the extent to which his conceptions could be
applied. But it is impossible not to view with admiration the
profound penetration, and the strictness of induction of so clear-
sighted a man, at a period when exact observations had been so few ;
he being the first to recognize the simultaneous effect of water and
heat in the formation of rocks, in imagining a system which embraces
* Fifth edition, p. 606.

ANNIVERSARY ADDRESS OF THE PRESIDENT. li

the whole physical system of the globe. He established principles,
which, in so far as they are fundamental, are now universally
admitted.”

I trust that I shall be pardoned in thus giving prominence to a
tribute offered, at this distance of time, by so eminent a foreign
geologist, to the genius and sagacity of Hutton, of whose ingenuity,
acuteness, and even light-hearted playfulness, I had been accustomed
in my early life to hear much in my own family, although too young
to have any personal intercourse with him; and in whose scientific
principles I was trained in my geological studies under the guidance
of my venerated friend the able and eloquent Playfair. I am, how-
ever, not prepared to agree with M. Daubrée that a shade has been
thrown over Hutton’s “noble conception ” that a continuous process
of decay and renovation of the materials of our globe had from the
origin of the stratified rocks been the established order of nature ;
that observations since the time of Hutton have demonstrated any
interruption to that continuity in ne time, or justify any anticipa-
tion of a future change.

In this work, as alll as in the more facant one of M. Delesse,
metamorphism is not limited to the class of rocks to which the term
metamorphic was originally applied: on the contrary, M. Daubrée
expressly says, “‘ Des effets de l’action métamorphique se montrent
dans les terrains de divers ages” (p. 119), and, at p. 74, that ‘les
dépéts metalliferes ne sont que des cas particuliers des phénomeénes
métamorphiques.” These three essays, in place of being called
«Etudes sur le Métamorphisme,” might have had, in my opinion,
the more appropriate and compr ehensive title of * Contributions to the
Chemistry of the Mineral Kingdom.” And most valuable contribu-.
tions they assuredly are; for the facts and experiments they narrate
enable us to form some just conception of the agencies by which the
lower sedimentary deposits became changed into hard and crystalline
rocks, and how their included accessory minerals may have been pro-
duced ; they are also calculated to throw light upon the analogous
changes of structure met with in the fossiliferous strata of all ages,
but which must have been produced undervery different circumstances,
and likewise upon the formation of the various products of mineral
veins. Even a short summary of the contents of these essays would
of itself amount to a treatise; so I must refer you to the works them-
selves, noticing only some of the conclusions of the authors to which
I wish to call your attention.

M. Delesse certainly states that the agencies in general metamor-
phism must have been heat, water, and pressure; but the main
feature in both his essays is the prominent part which he considers
water to have played in the production of mineral compounds. He
brings forward many facts for which the sole action of heat appears
to afford an inadequate explanation ; but, on the other hand, he seems
to be carried away by his theory to ascribe far too extended an
operation to aqueous causes. Thus, he affirms it as his opinion that
the trap of the Giant’s Causeway was not incandescent and in a
state of igneous fusion when it was poured over the lignite it covers ;
and in referring to the Meissner, near Cassel, so long celebrated as an.

liv PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

instance of the igneous origin of basalt, where a mass of it, in some
places 500 feet thick, covers beds of lignite from 20 to 98 feet in
thickness, he says that the phenomena exhibited are to be ascribed
“ plutot & une action aqueuse qu’a une action ignée.” Not only in
the above, but in other instances, he maintains the aqueous plasticity
of trappean rocks. Water may be one of their constituents; but it
is in no degree probable that it held the earthy constituents in a
softened, plastic, or fluid condition. It will require stronger proofs
than M. Delesse has as yet brought forward, to set aside the long-
established conviction of the similarity of origin of the Giant’s
Causeway and Fingal’s Cave to that of the columnar lavas of Etna
and Auvergne.

Although M. Daubrée does not carry his views of aqueous action
so far as M. Delesse does, he nevertheless expresses very decided
opinions as to the powerful agency of water in metamorphism, as the
following passage will show :—

‘Tt is, therefore, not difficult to see, in the various kinds of phe-
nomena of which [ have spoken, the manifestations of one and the
same agent, which exists throughout entire countries. That essential
agent is water, aided by heat of different degrees, and to which are
superadded as secondary causes, emanations which accompany it.
Thus we are of opinion that water acts unceasingly in the deep-
seated regions, after it has acquired a temperature more or less
elevated, under the influence of the heat of the globe.”—“ It cannot
be denied that if water is able to insinuate itself, through fissures in
the solid crust of the globe, to a depth equal only to that of the sea,
it becomes subject there to a pressure equal to several hundreds of
atmospheres, by means of which it will penetrate easily to the inmost
pores of the rocks, especially when it is of a temperature which it
must possess at such a depth.” (pp. 97 & 117.)

On this agency of water the following testimony of Prof. Bunsen
of Heidelberg is important:—“The attention of geologists has
hitherto been almost solely directed to the action of heat in the
production of the metamorphism of rocks. The action of gases and of
water at a moderate temperature in producing changes of structure,
which may be seen on a small scale in fumaroles, must have had
immense influence, as after-effects of older plutonic catastrophes,
upon the materials of which the stratified rocks are composed. In
this treatise I have endeavoured to bring forward some proofs and
circumstances which may perhaps set geologists upon the track of
those processes. Everything indicates that, in future, we must rely
not so exclusively on observation, but more upon experimental
researches to enable us to explain the metamorphism of rocks by
hydatothermic and pyrocaustic, or, where both have acted, by
hydatocaustic processes. I know not whether the time is yet arrived
for the introduction of those terms; but distinctions will be devoid
of meaning unless the test of experiment has determined their true
value, in every point of view*.”

* Bunsen, iiber den innern Zusammenhang der pseudo-vulkanische Erschei-
nungen Islands.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lv

Professor Naumann in his‘ Lehrbuch der Geognosie,’ the most
copious and instructive general treatise on geology with which I am
acquainted, briefly notices the conjectures of other geologists as to the
agencies in normal or general metamorphism, without expressing any
decided views of his own, except as to what heat may be supposed to
have effected. But he enters at considerable length into the subject
of abnormal or local metamorphism. He justly observes that while
here the origin of the effect is apparent, the modus operandi is far
from being equally so in a great proportion of cases. In the generality
of instances the heated state of the intrusive rock appears to have been
the cause; but he adds, “it is nevertheless evident that many of the
appearances when ordinary sandstones and quartzose conglomerates
are changed into quartzite by the contact of granite, syenite, and
other pyrogenous rocks cannot be explained by the action of heat
alone. For it is difficult to conceive that heat, which in its con-
tinuous state, at least, could not have been very great, and must at
all events be much under the melting-point of silica, could convert
a fragmentary sandstone into crystalline quartzite. It is clear that
such contact-metamorphism must belong to those instances the
production of which without the concomitant action of water is in-
conceivable *.”

There is an observation of M. Daubrée, which, so far as I know, is
novel and is well deserving of being followed up in researches in
metamorphism. He states that cases of the metamorphism of
sedimentary rocks occur only in those situations where disturbances
of the horizontality of such deposits have taken place: that the oldest
strata of Russia, Southern Sweden, and North America have preserved
their original horizontality and are not sensibly metamorphosed.
That, on the other hand, newer strata which have been much broken
up and elevated, such as the jurassic and cretaceous formations of the
High Alps, the Apuan and the Tuscan Alps, have been completely
modified, few only of the eruptive rocks being met with among them:
that clay-slates are but the beginning of more deeply-seated trans-
formations, and occur only in regions more or less disturbed: that
hot springs are always connected with accidents in the structure of
a country of a similar kind: that it is therefore difficult not to per-
ceive a connexion between the two phenomena, and no less difficult
to refuse one’s assent when we learn by experiment that the mineral-
ized waters are among the most energetic agents in that metamor-
phism which we can artificially produce7.

Gneiss is generally held to be a metamorphic rock, meaning thereby
that it was originally a sedimentary deposit of the detritus of a pre-
existent surface-rock, altered by subterranean heat as the chief
agent. There are, however, some considerations which make it
difficult for me to understand the modus operandi of this supposed
thermal action ; that is, in what manner the heat could be applied,
in accordance with known chemical laws. If gneiss be, as it is
usually held to be, the lowest known of the sedimentary stratified

* Lehrbuch der Geognosie, i. 793.
t Observations, &c. p. 38.

vi PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

rocks, it is obvious that it must necessarily have been formed by the
detritus of an original wnstratified surface-rock, which had been ex-
posed to the wearing effects of atmospheric action and of waves acting
upon a shore. The detritus, in order to form stratification, must
have been spread gradually over the solid bottom of a deep sea.

The generally prevalent theory assumes that the altering heat was
communicated through the rock on which the sediment rested, that
is, the sea-bottom. ‘Now unless we assume that the sca was in a
state of ebullition, the bottom rock must have been cold, by being in
immediate contact with cold water ; for so soon as the sea-water came
in contact with a heated mass, immediately there would be produced
two continuous currents, of ascending warm and descending cold
water, until the whole sea was raised to a high temperature. By
the pressure of the superincumbent water, the boiling-point in the
lower depths would be greatly raised, and the constant production
and upward direction of high-pressure steam would cause such a
turmoil in the sea that no tranquil deposition of sediment to form
stratification could possibly take place. If the source of heat were
local, the colder water from the adjoining parts of the seawould rush to
the heated parts. Ifthe bottom rock did not become heated until after
the sediment had accumulated to a great thickness, it is obvious,
from the very slow conducting power of rocks, that the lower parts, if
brought by the heat into such a softened state as to acquire a crystal-
line structure, must be very different in nature from the upper parts
of the deposit,—that, in short, there would be a gradual change in
the texture of the rock upwards—a difference which has nowhere
been observed. A similar difficulty attends the hypothesis in other
cases besides that of gneiss, when metamorphism is considered to
have been produced by sedimentary deposits having been acted upon
by a highly heated hypogene rock at the bottom of a sea.

As gneiss has never been seen to contain an undoubted fragment
of a pre-existent rock, nor any trace of an organism, its being held
to be an altered sedimentary deposit would seem to rest, first, on its
schistose and bedded structure, and, secondly, upon the extreme im-
probability of an eruptive rock having spread over vast regions with
that structure. As regards schistose and bedded strachines that is
of itself no conclusive proof. Gmeiss is essentially composed of the
same materials as eruptive granite, and there are numberless in-
stances, on a great scale, of a gradual passage from coarse-grained
granite into schistose gneiss. Some of these I will quote.

Dr. MacCulloch, in his ‘ Description of the Western Islands,’ when
treating of gneiss, which prevails in the Northern Hebrides, observes*
that there are two principal varieties, the one of a granitic, the
other of aschistose structure ; that the gneiss of these islands (Flan-
nan Isles) is in general composed of quartz, felspar, and mica ; that it
presents as usual many varieties, and among the rest, one sone can-
not be distinguished from common granite ; that this consists of an
equal mixture of flesh-coloured felspar, quartz, and but little mica,
forming beds among the rest of the rock; that there is not a trace

* Vol. i. pp. 202 & 226,

ANNIVERSARY ADDRESS OF THE PRESIDENT. lvii

of laminar tendency in their structure, and therefore, although they
may be considered as forming portions of the gneiss beds, they pre-
sent, in strictness, an example of bedded granite. He then goes
on to say that the limits which separate gneiss from granite are
evanescent, and that of this perpetual gradation there is scarcely a
mile of the survey of those islands which does not offer an example ;
that the granitic subdivision prevails, and is characterized not only
by a large grain and imperfectly foliated structure, but by frequent
transitions into granite, from which, when in detached specimens, it
cannot be distinguished.

As instances out of our owncountry of this intimaterelation between
varieties of gneiss and granite, I may give the following :—Carl von
Roemer, as quoted by Naumann*, while describing the northern side
of the central granite of Siberia, mentions an extensive tract of granit-
gneiss in which a laminar and bedded rock repeatedly alternates with
one of granular and massive structure without lamination ; and in like
manner, in Podolia, granite and gneiss form a massive, intermixed,
and compact whole, demonstrating a contemporaneityand similarity of
origin of both. Beudant states that in Hungary gneiss and granite
appear always together, and that they occur not only in alternating
beds, but as one and the same mass. Ele de Beaumont? states that a
passage between granite and gneiss, gneiss and mica-schist, and even
between granite and mica-schist, is so often observed as to prove, in
such cases, their common origin; that there are instances in which
it is evident that gneiss must have been an eruptive rock, which,
after its eruption, had been drawn out so as to assume a schistose or,
rather, a fibrous structure, so that it is often difficult to distinguish
petween the two kinds,—that is, between eruptive and metamor-
phic gneiss. M. Delesse says, that gneiss forms a transition be-
tween stratified and eruptive rocks ; that its mineralogical composi-
tion, as well as its mode of occurrence, unite it in a manner the most
intimate with granite, and that its origin is evidently the same.
The section of granite and gneiss at Jaegersborg, in Norway, given
by Mr. David Forbes§, proves indisputably, I think, that there the
two rocks must have had a common origin, and that it is not con-
ceivable that this gneiss can be an altered sedimentary rock.

When stratified gneiss contains, as it often does, a variety of ac-
cessory sunple minerals, and metamorphism by contact likewise pro-
duces them in the traversed rock, we have a complication of chemi-
cal action for a right understanding of which we must look to syn-
thetic experiment. Thus we know|| that, in limestones especially,
a great variety of minerals are often produced by the contact of
granite, among which garnet, idocrase, hornblende, wollastonite,
epidote, talc, chlorite, and zeolites are the most common. Now to
produce these eight minerals, there must be derived from the granite

* Lehrbuch der Geognosie, Ist ed. vol. ii. p. 84. UT oa Gan
t Etudes, &ec., 4to, p. 203.

§ Quart. Journ. Geol. Soc., vol. xv. p. 173.

|| Daubrée, Etudes et Expériences synthétiques, p. 57.

lviii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

and the limestone ten different elementary constituents, as the fol-
lowing table of the analyses of them shows :—

| PS hse
3 ae 2 Sel 6

; A= ®o |ke/Sal\ ew] # a Po
Ha Sa eI SSoPeet a oa | 2 | s
UREN TST aren Mace | eh |S te
a < xa eS |e rm raW & a & S

Garnet e:chec.scia: Fe ae aU SNe laser |e ioe
Idocrase............ 3 22 x * Fe Ne ee SERN ty *
Hornblende ...... % tee Ib ase * | x * * *
Wollastonite ...... See ee Bee see ooh ase Nd eee eae %

Epidote ............ x | «| ¥ | e | ¥ *

UA Kes aie aco acacia * * x % ee *
Chlorite .::.::5:.:.: * * * x *
ZeOMUES saesse5 dees * Ei eee a saat yore * *

It belongs to the chemist to show under what conditions these
elementary substances could, in the same mass, combine into. two
or more of those definite forms. They are phenomena of metamor-
phic action, of which, until explained, we cannot form any just con-
ception of that great operation of nature.

But there are accompaniments of many rocks that have received
the name of gneiss which would seem to favour the hypothesis of a
hypogene rather than a sedimentary origin, viz. intercalated masses
of granular and crystalline limestone, and metallic ores in masses
and disseminated through the substance of the rock.

MacCulloch describes* the gneiss of the island of Tiree as con-
taining masses of crystalline limestone, without stratification or con-
tinuity ; and it also occurs with a great variety of accessory erystal-
lized simple minerals in the gneiss of Norwayt, Sweden, Saxony,
Bavaria, Austria, and in different States of North America. Whence
the origin of this limestone thus contemporaneous with gneiss? It
cannot have been derived from the detritus of any surface-stratum ;
for no other than an eruptive rock could as yet have formed a part
of the dry land. If we could suppose it to be formed by the exuvize
of marine organisms, it would be carrying the prevalence of animal
life far beyond any period in which its existence has ever been con-
templated, except that Sir William Logan has suggested that nodules
of phosphate of lime found in sedimentary rocks of Lower Cambrian
or even greater age may have a possible connexion with life existing
at that very remote period of the earth’s history ; or if derived from
springs holding carbonate of lime in solution, that of itself would
be a proof of a hypogene origin. Many instances have been met
with of granular limestone occurring under circumstances that can
only be explained by supposing them to have had a subterranean
origin. Nearly forty years ago, Von Oeynhausen ¢ (elected a Foreign

* Description of the Western Islands, vol. i. p. 48.
t At Jaegersborg. See section by Mr. D. Forbes above referred to.
+ Noggerath’s Rheinland-Westphalen, vol. i. p. 163, 1822.

ANNIVERSARY ADDRESS OF THE PRESIDENT. lix

Member of this Society in 1827) described a dyke of great extent, com-
posed of saccharoid limestone, traversing a granitic ridge in the
Bergstrasse, between the villages of Auerbach and Schonberg ; it was
specially noticed by Von Leonhard* in 1833, who says of it, that
a close examination left the impression that it was erupted in a state
of igneous fluidity from the depths of the earth subsequent to the
formation of the gneiss ; for the granitic rock there appears both with
a gneissic structure and as syenite. And in 1852 Voltz? thus de-
scribes it :—‘‘ The whole appearance of the limestone is that of a
dyke ; and there can be no doubt that we have one of colossal size,—
the limestone being crystalline, and showing all varieties of structure
from fine-grained to caleareous spar.” Similar occurrences have been
described by Emmons in the State of New York, by Clarke in Au-
stralia, and by Dumas in the Cevennes{; and instances of veins of
large dimensions of calcareous spar, with numerous ramifications, ©
haying as much the appearance of injection from below as veins of
granite or trap, must be familiar to every geologist.

The gneiss of Norway and Sweden, in many parts, contains, dis-
seminated through the substance of the rock and in masses of vast
magnitude, ores of magnetic iron, of silver, copper, cobalt, zinc, and
arsenic; in Saxony it has been found containing tin, arsenic, iron,
and copper; in France, in the department of the Aveyron, it abounds
in magnetic iron ; and the same combination is met with in different
parts of the United States. These metallic minerals are surely
much more probably of subterranean than of sedimentary origin.

There is no manner of doubt that there are vast tracts of gneiss
with such distinct stratification, often greatly contorted, to which no
other than asedimentary origin can with any degree of probability
be ascribed, however difficult it may be, in the present state of our
knowledge, to comprehend the nature of the chemical action by which
the original component materials have been altered into new com-
binations. On the other hand, the assertion that all gneiss has
had the same origin appears to me erroneous, for the reasons I have
assigned ; and it is distinctly contrary to the opinion of some of the
most distinguished geologists of France and Germany.

A rock is now very commonly said to be metamorphic in such a
variety of cases, without any qualification of the term, whether in
relation to the nature of the materials acted upon, or to the totally
different texture of the rocks beneath, which have for hundreds or
thousands of feet undergone no similar alteration, that it is im-
possible to arrive at any other conclusion than that there must have
been different agencies at work—that the subterranean thermal
action considered to have produced gneiss from detrital matter could
not have produced the crystalline rock intercalated in a tertiary de-
posit. Palseontological determinations are made under the guidance
and control of the acknowledged laws of anatomy and physiology ;

* Neues Jahrbuch fiir Mineralogie, &c., 1833, p. 312.

+ Uebersicht der geologischen Verhaltnissen des Grossherzogthum Hessen,
p- 107.

¢ Naumann, Lehrbuch der Geognosie, 2nd edition, vol. ii. p. 88.

lx PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

so in cases of metamorphism chemistry must assert her authority.
If the term ‘metamorphic ” is to be used in any other sense than
merely as a synonym of the word “altered,” it is clear that:a wide
field of chemical research has to be cultivated before it can be justly
applied in a theoretical sense.

Endeavours to unravel the mystery of general metamorphism
may, at first sight, appear to be a hopeless task; and doubtless it is,
so far as regards the effects of a vast period of time. But by expe-
riments with the means within our power—that is, by heat, water,
and pressure, skilfully applied, under a variety of forms—we may
reasonably expect to acquire some just conception of the processes by
which mechanical detritus could have been converted into a homo-
geneous crystalline mass. Even as regards time, recent researches
have shown the contrast of the effects of the same agents when
brought shortly to a close and when they are prolonged for several
months. We must have multiplied synthetic experiments of the
kind of those instituted by Sir James Hall and Gregory Watt, and
since conducted with so much ingenuity and perseverance by Bischof,
Daubrée, Delesse, Sorby, and others; we must have it proved that,
by the combined action of heat, water, and pressure, something re-
sembling gneiss, mica-slate, clay-slate, and quartzite, with their
accessory simple minerals, may be formed out of sedimentary ma-
terials. But such experiments must, unfortunately, be of a kind and
on a scale that very few individuals can be expected to undertake ;
and they are therefore fit subjects for liberal grants from public
bodies entrusted with funds for the promotion of science.

I will now pass to a very different subject—to one which may be
said to have been for nearly two years the great geological question
of the day, and which has excited no small amount of general in-
terest,—the discovery of

Evidence of the early Existence of the Human Race.

Numerous newly discovered facts, and a more attentive and un-
prejudiced estimate of many of a similar kind, long since recorded,
seem to prove indisputably that Man must have been an inhabitant
of this earth at a far earlier period than we had been accustomed to
believe him to have existed. Ever since the discovery by Dr. Falconer
in 1858 of implements of human workmanship associated with the
bones of extinct quadrupeds in the cave at Brixham in Devonshire,
and the subsequent communication of Mr. Prestwich to the Royal
Society in May 1859, of his examination of the ground where M.
Boucher de Perthes had discovered, in a bed of gravel, flint hatchets
associated with the bones of extinct quadrupeds, at St. Acheul near
Amiens, and at Abbeville, this question has been a topic of intense
geological interest. Soon after the visit of Mr. Prestwich, to whose
paper in the Philosophical Transactions I must refer you for ample
details, M. Gaudry, a French geologist, went to St. Acheul, and in
two communications to the Academy of Sciences of France, on the
26th of September and 3rd of October, 1859, he gives the following
account of his researches :—‘“ The great point was not to leave the

ANNIVERSARY ADDRESS OF THE PRESIDENT. xi

workmen for a single instant, and to satisfy oneself by actual in-
spection whether the hatchets were found in situ. I caused a deep
excavation to be made, without quitting the workmen for a moment:
I found nine hatchets most distinctly in situ, in the diluvium, asso-
ciated with teeth of Hquus fossilis, and a species of Bos different from
any now living and similar to that of the diluvium and of caverns,
The exact determination of the position of the hatchets proves, be-
yond all doubt, that Man had been contemporary with several of the
larger animals that no longer exist, whose bones are now fossil.
One may easily be satisfied that the gravel beds are in their normal
state, and that they have not been remaniés by man. At St. Roch,
near St. Acheul, the diluvium has been found to contain remains of
the Rhinoceros tichorhinus, Elephas primigenius, and Hippopotamus ;
and M. Buteux has ascertained that the beds of diluvium of St. Roch
are continuous with those of St. Acheul*.”

On the 7th of last May, M. Beaudoin announced to the Geological
Society of France a discovery he had made of worked flints in un-
disturbed drift in the neighbourhood of Chatillon-sur-Seine; and on
the 20th of the same month M. de Verneuil communicated a similar
discovery at Precy, in the department of the Oise. Thus we have evi-
dence of the same event in the valleys of the Somme, the Seine, and
the Oise. More recently, M. E. Collomb, in a letter published in the
‘ Bulletin de la Société Vaudoise des Sciences Naturelles’ for October
1860, gives an account of a visit he paid to St. Acheul in company
with M. Lartet; and he fully confirms the accuracy of the observa-
tions of Mr. Prestwich and M. Gaudry, as to the age and undisturbed
condition of the gravel in which the worked flints are found. He
observes that almost the whole of the north of France, and especially
the plains, is in a condition the most favourable, the most normal,
for the study of the quaternary deposits (terrains quartaires), be-
cause, during that long period, no extraordinary events have occurred
in that region ; there have been no great cataclysms, no sudden ele-
vations or dislocations; no glaciers which could have broken up and
rearranged (remanié) the soil, and changed the regular order of the
superposition of the beds.

Additional evidence in support of the same views has been recently
supplied by the publication of a memoir communicated to the Society
of Antiquaries by John Evans, Hsq., a Fellow of this Society, who
accompanied Mr. Prestwich in his examinations at Abbeville and St.
Acheul. He states that he was himself witness to the extraction of
a worked flint from the gravel bed at St. Acheul, at a depth of 11
feet from the surface, and about 44 fect from the bottom of the pit;
—that, on another occasion, Mr. Flower, one of the party of geolo-
gists, uncovered and exhumed with his own hands a perfectly worked
instrument at a depth of 20 feet from the surface ;—that the imple-
ments occur most certainly in undisturbed gravel, for it is so hard
and compact as to require the use of a pickaxe, and therefore pre-
cludes all idea of its being a reconstructed mass ;—that there is
every improbability of the bones of extinct species of quadrupeds

* ‘Comptes Rendus’ of the above-mentioned dates.

Lxii PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

associated with the implements having been washed into the gravel
from an older deposit; for not only are they little if at all worn, but
in the lower beds at Menchecourt, near Abbeville, the skeleton of a
Rhinoceros was discovered nearly entire; and thus we have strong,
almost conclusive, evidence of the coexistence of Man with these
extinct Mammalia ;—that it appears to be established beyond a doubt
that, in a period of antiquity remote beyond any of which we have
hitherto found traces, this portion of the globe was peopled by Man ;
—that, at Amiens, land which is now 160 feet above the sea, and
90 feet above the Somme, has, since the existence of Man, been sub-
merged under fresh water, and an aqueous deposit from 20 feet to
30 feet in thickness, a portion of which at allevents must have sub-
sided from tranquil water, has been formed upon it; and that this
too has taken place in a country the level of which is now stationary,
and the face of which has been little altered since the days when
the Gauls and the Romans constructed their sepulchres in the soil
overlying the drift which contains these remains of a far earlier race
of men.

At a meeting of the Geological Society of France last April, at
which I was present, M. de Vibraye read an account of explorations
he had made in a cavern of jurassic rock near Arcy, in the Départe-
ment de l’Aube, between Troyes and Chalons-sur-Marne, which paper
has since been printed in the ‘ Bulletin’ of that Society. This cavern
contains three distinct beds of drift, the two uppermost bearing evi-
dence of remaniement; but the lowest he is satisfied must be an un-
disturbed mass of materials washed into the cavern by the same force
which spread the pleistocene drift, characterized by the remains of
fhinoceros tichorhinus, Ursus speleus, and Hyena spelca, over the
north-west of France. On making excavations in this lowest bed,
he met with a vast accumulation of the bones of the above animals ;
and among them, one of the labourers, while M. Vibraye was in the
cavern, found a human jaw. M. Vibraye thus describes this re-
markable event :—‘‘ Judge, gentlemen, of my surprise, when I saw
a human jaw. I felt disposed to doubt the reality, and to believe
that it was the jaw of an ape; but no, the doubt could not remain
for an instant; for the jaw, all the alveoli of which are perfectly
seen, still contained two well-characterized teeth, viz. the first right
lower premolar and the first large molar of the same side. I hastened
to satisfy myself not only as to the situation, but as to the actual .
place this important remain had occupied, and I can affirm that the
homogeneous bed, the lowest bed in the cavern, was perfectly intact,
and had in no respect changed its nature. I found this jaw while
devoid of all preconceived ideas, and was even obliged to do violence
to my individual convictions to admit the evidence. To add to the
value of this discovery, I ought to add that, while arranging the
numerous remains collected in this cavern during the last two years,
I found the tooth of another man, a first premolar of the lower jaw
belonging to an individual of less size than he to whom the jaw
belonged. This would tend to prove that the first discovery is not
an isolated fact, and that it is more than probable that further con-

ANNIVERSARY ADDRESS OF THE PRESIDENT. lxili

firmation would be found by continued researches.” The paper gave
rise to an animated discussion ; and M. Lartet, one of the speakers,
stated that he had visited the cavern, and had examined the collec-
tions of M. de Vibraye, whose identifications he confirmed, and that
he was of opinion that the drift in which they were found is of the
same age as that of St. Acheul.

The confirmation of the correctness of the conclusions to which
M. Boucher de Perthes had arrived, which he had published ten
years before, but which, by a strange unreasoning incredulity not
very creditable to the scientific men of all countries, had been suffered
to be neglected, is of an importance that cannot be overrated, inas-
much as it is calculated to remove a prejudice that has long prevailed
among geologists the least timid in forming conclusions, and as it bids
fair to eradicate one of a similar nature deeply rooted in the minds
of even the educated part of the general public.

It has been well remarked by the Rey. Mr. Kenrick, in his interest-
ing essay on Primeval History, that, ‘“‘ As we can assign no absolute
date to the introduction of man into the world, nor even decide with
confidence whether this took place by simultaneous or successive acts
of creative power, so it is impossible to define the time which he
occupied in adyancing from his primeval condition to that in which
he appears at the commencement of history*.” Now, although we
are unable to give any numerical expression to the time of the occur-
rence of events that have preceded all historical records of traditions,
we may arrive at a very firm conviction that they must have been ex-
tremely remote, by a consideration of the very slow process by which
changes take place on the surface of the land, and in the forms of
the coasts which are evidenily altered by the wearing forces of the
atmosphere and the sea, without any cataclysmal action. The long
duration of the vegetable soil and its covering of turf and forest, and
the resistance to the wearing effects of the weather by many human
works in stone have been well pointed out by M. Elie de Beaumont?,
He observes that plants fixing by their roots the superficial soil add
greatly to its stability,—that the natural state of the globe has been
to be coyered with yegetation,—that its surface has been covered by
turf or by forests,—that when we see turf on a mountain-slope we
may affirm that it has been almost coeval with the slope, and that
it has preserved the soil it covers for thousands of years,—that the
soil surrounding Cyclopean and Druidical monuments, which have
existed for more than 2000 years, has undergone no change either
of increase or decrease,—that the existence of a tree shows that the-
surface of the vegetable soil has undergone no sensible change during
the growth of the tree, and that there are trees which have existed
for many centuries.” Professor Phillips in his recent publication¢,
in reference to the slow process by which peat accumulates, has the
following passages:—‘ Man and the works of man haye been pre-

* An Essay on Primeval History. By John Kenrick, M.A, London:
Fellowes, 1846.

+ Lecons de Géologie Pratique, Legon 5.

¢ Life on the Harth, its origin and succession, pp. 48, 49. 1860,

xiv. PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

served in natural repositories of higher antiquity than all the mauso-
leums, and tumuli, and vzoyara,—in caverns, in peat-bogs, lacustrine
and river sediments, which derived their characteristic features from
the operation of physical conditions long since passed away. Thus,
deep in the sediments of many of our British valleys, left by the
rivers In some earlier period, we find the canoe of the primitive
inhabitant, hollowed by fire and rude stone chisels from the trunk
of the native oak.” <‘‘'T'o heap twenty or more feet of sediment over
the buried canoes by the ordinary operation of a river like the York-
shire Aire would require thousands of years: if it were not accumu-
lated under the ordinary circumstances now in operation, but under
different geographical conditions, this would perhaps require the
hypothesis of still longer time. In the alluvial sediments of this
same valley le nearly complete skeletons of the extinct Hippopo-
tamus major; in another place jaws and horns of the deer, and
hazel wood and nuts, some of them petrified. Perhaps Man was
contemporary with this extinct Hippopotamus, which has also been
found in the peat-deposits of Lancashire. The gravel of Amiens
and Abbeville appears to furnish evidence of a higher antiquity for
the flint implements found there.”

The discovery in Egypt of works of art executed more than 3000
years before our era, which could only have been produced by a
people arrived at an advanced stage in the slow process of civiliza-
tion (a conviction that has been strengthened by the recent discovery
of works of human art at great depths in the alluvial soil of the
Nile valley, which accumulates at the average rate of a few inches
in a century*) has been gradually producing an impression in the
minds of earnest thinkers that the first appearance of man on the
earth must be carried far beyond the time hitherto usually assigned
to it. When we come to reflect upon the geological changes that
have occurred in the configuration and structure of the country in
the north of France where the flint implements are found, proved
by the nature of the deposit in which they are met with and its
elevation above the sea-level, and take into account the length of
time which, according to all sound reasoning on geological phenomena,
we must assign for the accomplishment of those changes, the largest
sum of years which has been assigned for the existence of man in
Egypt can scarcely amount to more than a fraction of the time that
has elapsed since the men lived who chipped those flint implements.

The ground in which those worked flints were found at Amiens
‘and Abbeville is a part of a great post-pliocene deposit which is
spread over a great extent of the north of France, the geological age
of which is determined by the fragmentary materials, and by the
nature of the fossil remains of extinct species of quadrupeds. It is
marked in the geological map of France as composed of the group
designated the ‘* Alluviens anciennes de la Bresse, Sables des Landes,
Sables marins supérieurs de Montpellier,” resting upon another group
designated “ Fahluns, Meuliéres, Gres de Fontainebleau,” &e. That

* Memoirs on the Alluvial Land of Egypt, Phil. Trans. 1855, p. 105, and
1858, p. 53, by the Author.

ANNIVERSARY ADDRESS OF THE PRESIDENT, Ixy

part of it at St. Acheul consists of a bed of flint-gravel from 6 feet to
12 feet thick, resting on chalk. It was in this gravel that the
worked flints were found, and in the lowest part near the chalk. It
has been alleged that the gravel in this place is a case of what the
French call a remaniement, that is, an accumulation of the diluvial
gravel that had been disturbed by a local flood, or by man, which
involved in it the works of art belonging to a comparatively recent
time. But no evidence of this has been brought forward, and it has
been distinctly denied by M. Gaudry and Mr. Evans in the papers
quoted above. Other experienced geologists who have examined the
localities. both at Amiens and Abbeville, entertain no doubt that it
is an undisturbed deposit. I visited St. Acheul last April, and am
surprised that any one could see the least sign of a remaniement.

Another and a very decisive proof of the coexistence of Man with
extinct species of quadrupeds has been brought forward by M. Lartet,
a Foreign Member of our Society, in a paper read before us last May,
as well as in a communication in the same month to the Geological
Society of France. He there points out numerous instances of inten-
tional incisions by a sharp but rude instrument in such bones. These
incisions exist when the bones are disinterred ; and if the bones un-
questionably belong to extinct species, and if the deposit in which
they are found is certainly undisturbed ground, the evidence is com-
plete. All these conditions are fulfilled in the cases brought forward
by M. Lartet. He exhibited the specimens to myself in the Museum
of the Jardin des Plantes at Paris last spring.

To assign any approximate date for the age when the people who
formed these flint implements existed is impossible, in the present
state of our knowledge. But M. Lartet, who is not more distin-
guished by his paleontological knowledge than by habitual caution,
has not hesitated to express his belief on this subject in the following
terms in the paper in our Quarterly Journal I have already referred
to :—‘‘ M. d’Archiac has been led, by a series of well-weighed induc-
tions from stratigraphical considerations, to consider the epoch of the
separation of the British Islands from France as occurring after the
deposition of the diluvial rolled pebbles, and before that of the ancient
alluvium, the Loess of the north of France, of Belgium, the valley
of the Rhine, &c. The inference to be drawn from that hypothesis is
self-evident: it is this, that the primitive people to whom we attri-
bute the hatchets and other worked flints of Amiens and Abbeville
might have communicated with the existing country of England by
dry land, inasmuch as the separation did not take place until after
the deposit of the rolled diluvial pebbles, from among which the
hatchets and worked flints have been collected.”

Every geologist must be of the opinion of M. d’Archiac, that the
lands of England and France were once united—and that at no very
_ distant period in geological time, from community of structure and

from the occurrence of the remains of extinct species of quadrupeds
in England which could only have come to us over continuous land.
Mr. Evans, in the memoir above cited, states that the gravel at
St. Acheul closely resembles that on some parts of the Sussex coast,
and that the beds at the Moulin Quignon, near Abbeville, are nearly

VOL, XVII, é

ixvl PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

analogous to those near the East Croydon station and in many parts
of the valley of the Thames. The late Professor Edward Forbes, in
his remarkable paper on the Fauna and Flora of the British Isles
(pp. 343 & 346), observes that ‘no geologist doubts the ancient
union of the two sides of the Channel; ” and he considers that union
to have existed as late as the post-pliocene age; for he says that
“during the post-pliocene epoch, over the elevated bed of the glacial sea,
the great mass of the flora and fauna of the British Isles migrated
from the Germanic regions of the Continent.” We know that only a
very moderate change in the configuration of the two coasts has taken
place during the more than 1900 years since Julius Cesar crossed the
Channel. Even if the Channel was first formed by a sudden break
and sinking of the land, we cannot conceive so vast a gulf to have
been worked out into its present forms on both sides by the wearing
action of the sea, except during a period of vast duration.

The discoveries by Dr. Falconer and Baron Anca of siliceous stones
in forms that are evidently the work of man, mixed with the remains
of extinct species of quadrupeds, in the island of Sicily, are associated
with phenomena which indicate that a rupture in the continuity of
a continental land took place subsequently to the existence of man,
on a still greater scale than the channel which separates England
from France ; for they can only be explained by assuming that the
land now forming the island of Sicily was at that period a part of
the continent of Africa. Not only have bones and teeth of the ex-
isting African Elephant and Hyzena been found in great abundance,
but such enormous quantities of the bones and teeth of the Hippo-
potamus, that they were carried, for a short time, in ship-loads to
France, in the expectation that they might be used as agricultural
manure, until it was discovered that they were so far fossilized as to
have lost their gelatine. Now it is clear that the African Elephant
and Hyzena could only have come by land to those parts of Sicily
where their remains are now found. The distance between the
nearest part of Sicily and the coast of Africa, that is, between Mar-
sala and Cape Bon, is not more than about eighty miles ; and Admiral
Smyth, in his memoir on the Mediterranean, states (p. 499) that
there is a subaqueous plateau, which he named Adventure Bank,
uniting Sicily to Africa by a succession of ridges about a spot where
he found from 40 to 50 fathoms of water.

In a communication lately made to our Society by Captain Spratt,
relative to a cave near Kredi, on the south side of the island of
Malta, in which there was a stalagmitic bone-breccia, he informs
us that he discovered large quantities of the bones of the Hippo-
potamus. Malta is 58 miles from the nearest point of Sicily, and
179 from Cape Demos, the nearest point of the mainland of Africa.
Between Malta and Cape Passaro in Sicily, the charts give sound-
ings of 28, 62, 93, and 30 fathoms.

As the shaped stones are, in the opinion of Dr. Falconer and Baron
Anea, so associated with the bones of the quadrupeds as to lead to
the inference that the hands which fashioned them must have been
contemporaneous with the animals, that part of the human race must
have been in existence at the commencement of the time required

ANNIVERSARY ADDRESS OF THE PRESIDENT. Ixvil

to remove the greater part of the land now occupied by sea between
Sicily and Africa, Nor is this all; for if Dr. Falconer and Baron
Anea be right in their belief of Man having been a contemporary
with the Hippopotamus, the most probable explanation seems to me
to be this,—that since the commencement of man’s existence there
must have been a continent, now submerged, with the exception of
those parts of it that now form Sicily, Malta, and Gozo, through which
a great river flowed, in whose waters vast herds of those monstrous
animals swam, and on whose marshy banks they bred for successive
generations.

Modern discoveries in ethnology and philology afford cumulating
proofs of the very remote antiquity of the human race. The Rev.
Dr. Williams, in his review of Bunsen’s ‘ Biblical Researches,’ ob-
serves :— “There is no point in which archeologists of all shades
were so nearly unanimous as in the belief that our Biblical chro-
nology was too narrow in its limits; and the enlargement of our
views, deduced from Egyptian records, is extended by our author’s
reasonings on the development of commerce and government, and
still more of languages, and physical features of race. How many
years are needed to develope modern French out of Latin, and Latin
itself out of its origimal crude forms! How unlike is English to
Welsh, and Greek to Sanskrit, yet all indubitably of one family of
languages! What years were required to create the existing diver-
gence of members of this family! How many more for other families,
separated by a wide gulf from this, yet retaining traces of a primeval
aboriginal affinity, to have developed themselves, either in priority
or collaterally! The same consonantal roots, appearing either as
verbs inflected with great variety of grammatical form, or as nouns
with case-endings in some languages and with none in others, plead
as convincingly as the succession of strata in geology for enormous
lapses of time*.”

There undoubtedly exists a widespread belief that the first ex-
istence of man belongs to a period not very remote from history or
tradition. Every discovery which threw a doubt on the correctness
of that belief was, until very recently, regarded, even by well-
instructed geologists, as an imperfect observation, im which con-
comitant circumstances had been overlooked, which would have
shown that the inference of a great antiquity was erroneous ; nor
have those who were led to make such inferences been always
exempt from the charge of irreverently maintaining opinions at
variance with Sacred Writ. To what cause can we ascribe this
incredulity? How does it arise that, while the statements of
geologists that other organic bodies existed millions of years ago are
tacitly accepted, their conclusions as to man having existed many
thousands of years ago should be received with hesitation by some
geologists, and be altogether repudiated by no inconsiderable number
among other educated classes of society? It is true that negative
proof is brought forward that human bones have never been found
associated with those of extinct animals; but granting this to be
correct, which recent discoveries show that it is not (and the rarity

* Hssays and Reviews, p. 54. London, 1860.
e2

lxvili PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

of their occurrence is capable of bemg accounted for on many rea-
sonable grounds), still against such merely negative evidence we
have undeniable proofs, in numerous places, of the existence of such
an association with man’s works, and even many instances of his
haying applied the bones of such animals to his wants. My own
conviction is, that this wide-spread belief of the recent existence of
man is to be ascribed, so far at least as this country is concerned, to
the impression made by the lesson taught in early youth, the sound-
ness of which is not questioned in after-life, by that marginal note
in our Bibles over against the first verse of the first chapter of the
Book of Genesis, that ‘‘ In the beginning God created the heaven and
the earth” [ four thousand and four years before the birth of Christ].
It is more than probable that of the many millions of persons who
read the English Bible, a very large proportion look with the same
reverence upon that marginal note as they do upon the verse with
which it is connected.

It will be useful to look into the history of this date of 4004
years, given, with so much precision, for the creation, not of this
our earth only, but of the universe, and to inquire into the authority
by which an addition of so much import is made to the sacred text.

The author of the chronology given in the margin of our Bibles
was Usher, Archbishop of Armagh. I make no allusion to any part
of the learned prelate’s system, except the date he assigns for the
creation of the world: that date comes properly within the province
of the geologist ; for, as the almost religious belief in its accuracy is
an obstacle to the acceptance of the conclusions to which he is led by
a careful study of the facts which the structure of the earth exhibits,
he is fairly entitled to deal with it.

In the eighth volume of the Archbishop’s Works*, there is a
treatise with the following title :—‘ Annates VeTeris TESTAMENTI, @
prima mundi origine deducti, and in p. 13 of that treatise we find
the following sentence :—“ In principio creavit Deus ceelum et terram,
quod temporis principium, juxta nostram chronologiam, inceidit m
noctis illius initium, que vigesimum tertium diem Octobris preecessit,
m anno periodi Juliane 710.’ Then follows :—‘ Primo igitur secult
die, Octobris vigesima tertia, feria prima, cum supremo celo ereavit
Deus angelos: deinde summo operis fastigio primum perfecto, ad ima
mundane haus fabrice fundamenta progressus mirandus artifex,
infimum hune globum ex abysso et terra conflatum constituit.”

In the eleventh volume of the same edition of the prelate’s works
there is a treatise with the title—‘CHronoLoerA Sacra,’ in the
second chapter of which the Archbishop thus settles the number of
years, before the birth of Christ, for the creation of the world :—
“Tta a vespera primum mundi diem aperiente, usque ad mediam
noctem initium prebentem, 25. quidem drei Decembris, quo Christum
natum supponimus, annos Julianos 3999. menses rpraxovOnpepous 2.
dies 4. et horas 6. Kalendis vero Januariis anni periodi Juliane
A714. (a quibus vulgaris ere christiane exordium deducimus) annos
4003. menses 2. dies 11. et horas 6. decurrisse colligimus.” This,
therefore, is the authority upon which the confident belief is founded,

* Edition printed at Dublin in 16 vols. 8vo.

ANNIVERSARY ADDRESS OF THE PRESIDENT, lxix

that man could not possibly have existed upon the earth for a longer
period than considerably less than 4000 years B.c.

But this determination of the Archbishop is only one of many
dates which chronologists, in their vain calculations, have presumed
to assign to this the most stupendous of all events, to attempt to
form a faint idea of which, in anything relating to it, will ever be
gross presumption and folly. In the well-known work, ‘ L’Art de
vérifier les Dates,’ the following passage occurs :—‘‘ Les chronolo-
gistes sont loin d’étre d’accord sur le nombre des années du monde.
Desyignoles (Chronologie de l’ Histoire Sainte, préface) assure qu’il a
recueillé plus de 200 caleuls différents, dont le plus court ne compte
que 3483 ans depuis la création jusqu’a l’ére vulgaire, et le plus long
en suppose 6984.” There then follows a “ Table des années écoulées
depuis Adam jusqu’a la naissance de Jésus Christ, selon le calcul
des principaux chronologistes,” numbering 108, beginning with

‘« Alphonse X, roi de Castille, mort le 24 Avril 1284, dans

les Tables de Jean Miller, appelé aussi Regiomontanus 6984,”

and ending with

“Louis Lippoman, savant Vénitien, mort en 1554..... 3616.”

The Rev. Dr. Hales, in his ‘New Analysis of Chronology,’ gives
a similar list of ‘‘ Epochs of the Creation,’ and adds :—‘ Here are
upwards of 120 different opinions, and the list might be swelled to
300. This specimen, however, is abundantly sufficient to show the
disgraceful discordance of chronologers even in this prime era.”

I have endeavoured, by inquiries at Oxford, Cambridge, Edin-
burgh, and at the Queen’s printers in London, to ascertain by what
specific authority, Royal or ecclesiastical, the date of 4004 was
added to the first verse in Genesis in the authorized version, and
I have not been able to discover that any record exists of such an
authority. In Lewis’s ‘Complete History of the Translations of the
Holy Bible into English*,’ it is stated, in p. 349, that, to an edition
in folio of the Bible, published in 1701, under the direction of Arch-
bishop Tenison, Dr. Lloyd, Bishop of Worcester, added chronological
dates at the head of the several columns, and on the margin of the
title of Genesis the following :—‘“ Year before the common year of
Christ, 4004.’’ This edition is to be seen in the British Museum:
it was “‘ printed by Charles Bill and the executrix of Thomas New-
comb, deceased, printers to the King’s Most Excellent Majesty.”

The copy of the Bible in the Bodleian Library, Oxford, in which
that date first appears over against the first verse of Genesis, bears
the date of 1727; but there is no doubt that for more than a cen-
tury and a half that unauthorized marginal note has been added, up
to the present time’.

* By John Lewis, A.M., 1738. New edition, London, 1818.

+ In the Royal Library at Berlin, I last summer found a folio Bible, printed
at Liége in 1702, being a French translation with the Latin Vulgate side by side,
and over against the first verse of the first chapter of Genesis there is printed in
the margin 4004 years for the creation of the world.

Editions of the Bible with marginal notes, printed at Oxford and Cambridge
in the year 1858, and an edition by the Queen’s Printer in London, with the
date of 1860, have the same date for the same event.

lsxexe -PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

I have thus laid before you the origin of this settled point in Sacred
History as taught at this day in our schools*, and, from its juxta-
position to the text of the Bible, held in veneration by millions, there
is every reason to believe, as an undoubted truth. The study of
geology has become so general that those who are instructed in its
mere elements cannot fail to see the discrepancy between this date
and the truths which geology reveals. The youth is told in the
morning at school, probably by his own minister of religion, as I
myself have witnessed, that not more than about 6000 years have
elapsed since the creation of the world. In the evening he may
attend a lecture on geology, very possibly by one of the ninety-three
clergymen who are Fellows of this Society, and hear that, in a work
just issued from the press (a Lecture by a Professor in the University
of Oxford, delivered before the Vice-Chancellor of the University of
Cambridge), it is stated that “ the probable length of time required
for the production of the strata of coal, sandstone, shale, and iron-
stone in South Wales is half a million of yearsy.” It is thus easy
to see what a confusion must be created in the youth’s mind, and
that he will involuntarily ask himself, ‘“‘ Which of the two state-
ments am I to believe?” ‘There can be very little doubt what his
decision would be ; for he found the lecturer resting his statement on
unmistakeable records preserved in the great book of Nature, the
genuine incorruptible register of God’s works; whereas his school
instructor had adduced no evidence from the sacred text for his
averment. ‘To remove any Imaccuracy in notes accompanying the
authorized version of our Bible is surely an imperative duty. The
retention of the marginal note in question is by no means a matter
of indifference: it is untrue, and therefore it is mischievous. If in
future editions this erroneous date be removed, the omission of any
other will best express that entire ignorance of ‘‘ The Beginning ”’
which no human power will ever be able to dispel.

I cannot conclude this subject better than by quoting the eloquent
words of one of the most able and accomplished of our Associates,
the Rev. Adam Sedgwick, who, in the Appendix to his Discourse
on the Studies of the University of Cambridge, thus expresses
himself + :—

* Between the first creation of the earth and that day in which
it pleased God to place man upon it, who shall dare to define the
interval? On this question Scripture is silent; but that silence de-
stroys not the meaning of those physical monuments of his power
that God has put before our eyes, giving us, at the same time,
faculties whereby we may interpret them and comprehend their
meaning. In the present condition of our knowledge, a statement

* The event is so recorded in three school histories of the Old Testament now
selling at the Book Depository of the National Society for Education of the
Established Church. In a school-book with the title of ‘Scripture Lessons,’
published by direction of the Commissioners of National Education in Ireland,
“Tine Creation, B.c. 4004,” stands at the head of the First Lesson; and in the
preface it is stated, “These Lessons, as the name imports, are drawn from the
Sacred Volume.”

t Professor Phillips, ‘ Life on the Earth,’ p. 134.

{ Fifth edition, 1850, p. 110.

ANNIVERSARY ADDRESS OF THE PRESIDENT, lxxi

like this is surely enough to satisfy the reasonable scruples of a
religious man. But let us, for a moment, suppose that there are
some religious difficulties in the conclusions of geology. How then
are we to solve them? Not by making a world after a pattern of
our own, not by shifting and shuffling the solid strata of the earth,
and then dealing them out in such a way as to play the game of an
ignorant hypothesis; not by shutting our eyes to facts, or denying
the evidence of our senses, but by patient investigation, carried on
in the sincere love of truth, and by learning to reject every conse-
quence not warranted by direct physical evidence. Pursued in this
spirit, geology can neither lead to any false conclusions, nor offend
against any religious truth.”

Appendix to Mr. Horner’s Anniversary Address.

Tn stating the evidence for the early existence of the Human Race,
I give a passage from an essay by Dr. Williams, to show that modern
discoveries in ethnology and philology afford cumulating proofs of
the very remote antiquity of man. When that paragraph was printed
I had not seen an unpublished memoir, entitled ‘ On the Antiquity
of Man, from the evidence of Language,’ by John Crawfurd, Esq.,
F.R.S., President of the Ethnological Society, and author of ‘ The
Grammar and Dictionary of the Malay Language,’ published in
1852. From that memoir I quote, with the permission of the author,
the following passages :—

« The periods usually assigned for Man’s first appearance on earth
necessarily date only from the time when he had already attained
such an amount of civilization as to enable him to frame some kind
of record of his own career, and take no account of the many ages
which must have transpired before he could have attained that
power. Among the many facts which attest the high antiquity of
Man, the formation of language may be adduced, and in the course
of this short paper, I shall endeavour to bring forward a few of the
most striking facts which it yields.

« Language is not innate, but adventitious—a mere acquirement,
haying its origin in the superiority of the human understanding, like
any other acquisition derived from the same source. The evidence
that such is the case is abundant. Infants are without language,
and we see them slowly and gradually attaining it, in proportion as
the brain acquires maturity. Children acquire with equal facility
any language whatsoever; they can forget the first acquired lan-
guage, and learn another.

«* Among the unquestionable proofs that language is not innate,
is the prodigious number of languages which exists,—some with a
yery narrow range of articulate sounds, others with a very wide one ;
some with words confined to single syllables, and others having
many; some being of very simple, and others of a very complex
structure. Such a state of things necessarily implies that each
tongue was a separate and distinct creation, or that each horde
framed its own independent tongue.

«« Tf additional confirmation of the fact that lameueeen Is an adven-

xxii PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

titious acquirement were wanting, it will be found in this, that a
whole nation may lose its original tongue, and in its stead adopt any
foreign one. The language which was the vernacular one of the
Jews 3000 years ago has ceased to be so for above 2000, and the
descendants of those who spoke it are now speaking an infinity of
foreign tongues,—sometimes European and sometimes Asiatic.
Languages derived from a single tongue of Italy have superseded
the many native languages which were once spoken in Spain, in
France, and in Italy itself. A language of German origin has nearly
displaced, not only all the native languages of Britain and Ireland,
but the numerous ones of a large portion of America. Some eight
millions of negroes are planted in the New World, whose forefathers
spoke many African tongues. These African tongues have nearly
disappeared, having been supplanted by idioms derived from the
German and Latin languages.

“« It necessarily follows from what has now been stated, that Man,
when he first appeared on earth, was destitute of language. He had
to frame one: each separate tribe framed its own, and hence the
multitude of tongues. However difficult may appear to us the task
of framing a language, there can be no doubt that in every case the
framers were arrant savages, which is proved by the fact, that the
rudest tribes ever discovered had already completed the task of
forming a perfect language. The languages spoken by the grovelling
savages of Australia are in this state, and even more artificial and com-
plex in their structure than those of many people far more advanced.

“The first rudiments of language must have consisted of a few
articulate sounds in the attempts made by the speechless but social
savages to make their wants and wishes known to each other; and
from these first efforts to the time in which language had attained
the completeness which we find it to have reached among the rudest
tribes ever known to us, countless ages we must presume to have
elapsed.

«In every department of language we find evidence of the great
antiquity of man. Between the time, for example, when men had ac-
quired the art of fashioning a club, of kindling a fire, and of making
a flint knife, and that in which writing was invented, many ages
must have passed. The conditions of quality of race and of local
advantages must have been propitious to allow of the discovery
having been at all; and so we find that it never has been made
where these were not favourable.

«The Egyptians must have attained a large measure of civiliza-
tion before they had invented symbolic or phonetic writing, and yet
we find these in the most ancient of their monuments. ......

«« From the sketch which I have now given of the formation of
language, the conclusion is, I think, inevitable, that the birth of Man
is of vast antiquity. He came into the world without language, and
in every case had to achieve the arduous and tedious task of con-
structing speech which, in the rudest form in which we find it, it
must have taken many thousands of years to accomplish.”—L, H.
March 26, 1861,

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

THE GEOLOGICAL SOCIETY.

Novemser 7, 1860.

Wiliam T. Blanford, Esq., of the Geological Survey of India ;
the Rev. Thomas Bigsby Chamberlin, Kirton-in-Lindsey, Lincoln-
shire ; James Sparrow, Esq., Cymmau Hall, near Wrexham ; and
Richard Fort, Esq., Read Hall, near Whalley, Lancashire, were
elected Fellows.

The following communications were read :—

1. On the Denvpation of Sorr Srrata.
By the Rey. O. Fisuer, M.A., F.G.S.
( Abstract.)
Tue author first described the general features of the north-eastern
portion of Essex, which consists, in part, of table-lands of gravel,
with valleys cut into the subjacent London Clay and terminating
seaward in tidal rivers, and, in part, of a gently undulating surface
of London Clay, from which the gravel has been mostly swept clean
away, except in places where flat outlying tracts of gravel still
remain: these features extend also into the neighbouring county
of Suffolk. The tidal rivers are evidently nothing more than a con-
tinuation of the valleys beneath the sea-level; and the same may be
said of irregularly shaped inlets of the sea, like that behind Walton-
on-the-Naze, which is a submerged valley in the part of the district
where the surface is composed of London Clay.
The present configuration of such a district cannot be due, in the
author’s opinion, to the action of such causes as we now see in

operation on the coast combined with a slow and continued elevation
VOL. XVII.—PART I. B

ae

2 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 7,

of the land. Sea-waves cannot excavate long narrow inlets in ho-
mogeneous beds (such as Chalk), nor in horizontal beds, such as the
gravel and clay of the district under notice; for the effect of sea-
waves is to form long and approximately straight lines of cliff. Any
curvature seen in such a line of cliff will be found to be due to some
disturbing cause, as a variation in the resisting power of the strata,
or the set of a current, or exposure of some parts to a greater force
of wind, in which cases a bay will be formed, but not a long and
winding creek.

If it were possible (which the author denied) for such valleys as
those of the district under consideration to be formed by wave-
action, their sides should present the appearances of degraded cliffs,
masked with a talus of gravel derived from their crests; mstead of
which, their sides are rounded, the gravel-beds thinning out at the
hill-top, and the clay exposed on the sides ; nor is there any evidence
of the existence of shingle-beds at the foot of the hills.

The only other agency of an ordinary character to which such
denudation could be attributed seems to be tidal action, either at a
time when the district was under water, or else during a gradual
rise. But it seems impossible that the diurnal slow passage of a
body of water to and fro over a sea-bottom could sweep out diverging
narrow channels, carrying clean away gravel charged with large
pebbles. Nor does the second supposition seem more favourable for
the purpose, because the rapidity of the current in the tidal portions
of the rivers, as we see them, is not competent to do more than to
keep clear a comparatively narrow channel in their centres, the sides
becoming covered with a deposit of mud (dry at low water), which,
in the upper portions, forms alluvial tracts of meadow-land; nor does
there seem any reason why the denuding power of the tidal rivers,
during a gradual rise, should be greater than at present.

Mr. Fisher does not see any other way of accounting for such a
form of surface as obtains in this district, and in many others com-
posed of yielding strata, than by a superincumbent mass of water
rapidly draining off from a flat or shghtly dome-shaped area. Slight
depressions, cracks, or lines of readily yielding materials would first
determine the course of the streams of drainage; and these would
cut channels which would be more or less completely scoured out
according to the velocity of the water. Where the gravel-covering
of such a district was cut through, the clay beneath would be chan-
nelled with a narrower and deeper valley,—the cutting power of the
water being also assisted by the gravel hurried along with it; and
where the gravel was wholly removed, the valleys would be wider,
and the intermediate high ground rounded instead of being flat-
topped. This character of surface is seen in the most eastern portion
of Essex, and in nearly all clay-districts which are not low and flat.

The surface of the mud of a tidal river left dry at low water shows,
on a small scale, a configuration identical with that described, and
clearly due to the draining off of the superincumbent water when
the tide falls. The only difference in the mode of action is that, in
this case, sediment, instead of being swept away, after having been

1860. ] FISHER—-DENUDATION. a

deposited, is not permitted to accumulate, so that a slower movement
of the water is effectual daily to clear out the little valleys. These
valleys in the surface of the mud are not formed by wavelets, which,
at low water, begin to cut a miniature straight cliff at the margin of
the mud. :

These arguments lead the author to infer that the land must have
been elevated by a sudden movement sufficient to have caused a
rush of water from the raised portions to seek a lower level,—either
the land being raised high and dry at once, or the sea-bottom raised,
though still remaining beneath water. Such an elevation might be
repeated again and again with intervals of submergence; and many
of the phenomena connected with sunk forests, and other Pleistocene
phenomena, seem to show that such conditions have really obtained
in places at considerable distances apart.

The author stated that, in his opinion, escarpments, such as are
so common among the secondary and tertiary strata, are rarely old
cliffs, and he thinks that their rounded forms are due to such agency
as he has described. In forming this opinion, he relies upon the
following arguments :—

Cliffs in the softer beds run in approximately straight lines, or
sweeping curves, while escarpments abound in nooks and combs
running up into the hill-face (according to his view, gullies), down
which the water has poured where it happens to have broken through
the crest. Again, a line of cliff usually cuts off stratum after stratum,
while the line of an escarpment usually follows the course of one
stratum, and is entirely determined by the intersection of an approxi-
mately constant level with its undulating surface, that level rising
slightly where the stratum is harder, and sinking where it is softer.
Again, in an escarpment, like those of the Chalk, the mouths of the
valleys run down into the plain below; but in a cliff many valleys
are seen to be cut off at a level considerably above the beach,—a
condition which would be clearly marked in a hill-side which had
formerly been a cliff. The author cannot remember to have ever
seen such a termination to a valley in the face of a Chalk or other
escarpment.

Proofs of torrential action in Chalk-districts were referred to,—
for instance, the perfect drainage-system of the dry valleys of Salis-
bury Plain and other extensive tracts of Chalk-downs, the loose
flints filing the bottoms of such valleys, and the immense blocks of
tertiary pudding-stone and “ Druid-sandstone,” scattered along the
bottoms of Chalk-valleys, as in the Portisham and Bridehead valleys
near Weymouth, and the Marlborough “ Wethers” in Wiltshire.
Mr. Fisher also thinks that he sees evidence of the friction of a
great body of water rushing down a hill side in the manner in which
vertical or nearly vertical strata are usually bent over at their ex-
posed edges.

In estimating the denuding power of such a cause as that sug-
gested, it is evident that the effects would be least of all on water-
sheds, great at the crests of valley-sides, and greatest of all in their
bottoms, and that, where the velocity was diminished from any

BZ

4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 7,

cause, sediment and brick-earth would be left behind. The author
also sees an agency competent to deposit an extensive spread of
brick-earth in the unlading of icebergs,—the coarser gravel sinking
more quickly, and the finer particles and angular splinters less
readily, and being lable to be stirred up and raised higher by every
fresh shower of gravel falling upon them.

The author, having shown that the contour of the existing surface
of our softer strata and other observed phenomena seem due to the
sudden uprising of the land from beneath the sea, next inquires
whether there have been more than one such movement, and whether
these have been combined with periods of depression. Without en-
tering into any detail on this part of the subject, he remarked that,
the present contour being in the main the same as it was at the
period of the great-mammalian fauna (only less elevated), there
must have been a sudden elevation preceding that period, and that,
during subsequent depressions, the valley deposits were formed in
which the mammalian bones le entombed, the valleys haying been
again partially re-excayated by the repetition of a sudden but less
lofty upheaval.

Lastly, it was pointed out that sudden vertical movements of the
surface on a grand scale are of as probabie occurrence as those lesser
movements with which we are historically acquainted ; for the earth’s
crust, to the depth of at least many miles, is rigid to such a degree
that great changes of position in its parts cannot occur without
actual disruption of the strata, as all faults testify. Its movements
are not those of a flexible or semifluid envelope. Now, the pres-
sure requisite to rupture nearly rigid strata will accumulate enor-
mously before they yield to it, causing probably a slow and gradual
movement from the want of absolute rigidity; but when once they
are ruptured, they will be thrown up or down with a sudden move-
ment. This will be true even on old lines of fault, for it will require
u great and new accumulation of force to overcome the friction on
the line of fault; but when once the rocks are set in motion, the
resistance caused by the friction will be much less, according to a
well-known principle in mechanics. Again, if lateral pressure,
arising from failure of support, be the nature of the force which has
elevated tracts of the earth’s surface (which is the author’s persua-
sion), such a pressure might accumulate very greatly without pro-
ducing any vertical movement; but as soon as any local circum-
stance determined the course of an anticlinal or fault, the edges of
the strata on one or both sides of that line would begin to be raised
with reference to the neighbouring parts, and the pressure which, as
in a bridge, had long existed in the plane of the crust without pro-
ducing motion, would now act at an angle to the beds with momen-
tarily increasing advantage, as in a bridge beginning to fall, tilting
them into inclined positions, probably crushing them, and producing
minor dislocations at the same time.

Thus, by mechanical considerations, the author is led to believe
that the ordinary nature of the greater movements of the earth’s
crust must be sudden.

1860. | DAWSON—FOSSIL FERN. 5)

2. On an UnvEscrisep Fosstt Fern from the Lower Coat-MEasures
of Nova Scotia. By Dr. J. W. Dawson, F.G.S.

(Abstract. )

In a paper on the Lower Carboniferous rocks of British America,
published in the 15th volume of the Geological Society’s Journal,
Dr. Dawson noticed some fragmentary plant-remains which he re-
ferred with some doubt, the one to Schizopteris (Brongn.), and the
other to Sphereda (L. and H.). With these were also fragments
of a fern resembling Sphenopteris (Cyclopteris) adiantoides of Lindley
and Hutton. Since 1858 the author has received a large series of
better-preserved specimens from Mr. C. F. Hartt; and from these he
finds that what he doubtfully termed the frond of Schizopteris is a
flattened stipe, and that the leaflets which he referred to Sphenopteris
adiantoides really belonged to the same plant. Mr. Hartt’s speci-
mens also lead Dr. Dawson to suppose that what he thought to be
Spherede were attached to the subdivisions of these stipes, and may
be the remains of fertile pinne, borne on the lower part of the stipe,
as In some modern ferns. ‘This structure he regards as being some-
thing ike what obtains in the Cuban Aneimia adiantifolia, as pointed
out to the author by Prof. Eaton, of Yale College. No sporangia
are seen in the fossil specimens.

Dr. Dawson offered some remarks on the difficulties of arranging
this fern among the fossil Cyclopterides, Neeggerathice, and Adian-
tates; and, placing it in the genus Cyclopteris, he suggested that it
be recognised as a. subgenus (Aneimites) with the specific name
Acadica.

The regularly striated and gracefully branching stipes, terminated
by groups of pinnules on slender petioles, must have given to this
fern a very elegant appearance. It attained a great size. One
stipe is 22 inches in diameter, where it expands to unite with the
stem; and it attains a length of 21 inches before it divides into
branches. The frond must have been at least 3 feet broad. The
specimens are extremely numerous at Horton.

The author then noticed that the long slender leaves so common
in the Coal-measures of Nova Scotia, and hitherto called Poacites,
though sometimes like the stipes of Anevmites, are probably leaves of
Cordaites.

On some specimens of Cyclopteris (Aneimites) Acadica, markings
like those made by insects have been observed ; also a specimen of the
Spirorbis carbonarius.

6 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 7,

3. On the Suctions or Strata exposed in the Excavations for the
Sourn HieH-LeveL Sewer at Dutwicu ; with Notices of the Fossits
found there and at Pecknam. By Cuarzes Rickman, Esq.

(Communicated by the Assistant-Secretary.)
(Abstract.)

Ty the autumn of 1859, open cuttings were made at Peckham, in
connexion with the “ Effra branch of the Great South High-level
Sewer,” for the “‘main drainage” of the metropolis south of the
Thames; and in the following spring a tunnel (330 yards in length)
was being constructed under the Five-fields at Dulwich. The beds
exposed in both sections belong to the ‘‘ Woolwich and Reading
Series’ of the Lower London Tertiaries (Prestwich).

Four shafts were sunk to facilitate the driving of the tunnel; and
the following beds were expesed ; but, as some of the beds are not
persistent, but die out even within the extent of the tunnel, the
several shafts differed as to the sections obtained from them.

1. Soil, 9 inches. 2. Loamy clay (probably London Clay) ; 12 ft.
Not in shaft No. 1 (the most easterly), nor in No. 4 (the most
westerly), owing to the convex surface of the ground. 3. Light-
coloured clay; 6 to 9ft. 4. Reddish sand; 5 ft. (not in No. 4 shaft).
5. Dark clay; 1 ft. 10in. 6. Blue clay; 2 ft. (mot in No. 4). 7.
Dark clay ; 1 ft. (in No. 1 only). 8. Paludina-bed ; 6 to 15 inches.
[ Fossils: Pitharella Rickmani (Edwards), Paludina lenta, P, aspera(?).
Bones and scales of Fish. Leaves.| 9. Cyrena-bed; 1 to 2 ft.
[Cyrena cuneiformis, &c.| 10. Oyster bed; 1 to 3 ft. [ Ostrea tenera,
O. pulchra, O. Bellovacina, O. elephantopus, O. edulina, Bysso-arca
Cailltaudi (2), Cyrena cuneiformis, C. deperdita, C’. cordata, C. 0b-
ovata, Melania inquinata, Melanopsis brevis, Modiola elegans, Fusus(?),
Calyptrea trochiformis, Corbula.| 11. Loamy sand ; 8 in. (in No. 4
only). 12. Red sand; 2 ft. (in No.4 only). 13. Blue clay ; 2 ft. 6 in.
[Leaves.] 14. Dark sand; 8 to 28in. 15. Blue clay; 18 in. to
9ft. [Laminated; rich in Leaves, Lignite, Seed vessels. Rissoa, ~
Cyrena Dulwichensis (Rickman).| 16. Dark sand; 2 to 4ft. 17.
Light-coloured clay ; 2 ft. 6 in. (in No. 4 only). 18. Shell-rock ;
4 ft. thick, sometimes intercalated with stiff blue clay. [Cyrena
Dulwichensis (Rickman), C. cordata, C. deperdita, C. cunetformis,
Melania inquinata, Melanopsis, Neritina, Pitharella Rickmani (Ed-
wards), Unio, Teredines in Lignite, Secutes of Crocodile, Fish-scales,
Chelonian and Mammalian bones.| 19. Clay; 14 ft. and more:
reached only by the main shaft, No. 3, which appears to have been
sunk at the apex of a low anticlinal; the beds gently dipping away
KE. and W.

All the fossils appear in their respective beds both at Peckham
and Dulwich.

1860. ] FORBES—BOLIVIA AND PERU. a

NovremBer 21, 1860.

Robert Jones Garden, Esq., 63 Montagu Square; and Robert
Home, Lieut. R.E., Royal Staff-College, Sandhurst, were elected
Fellows.

The following communications were read :—

1. On the Grotoey of Boxtvia and SourHEeRN Perv.
By Davin Forsgs, Esq., F.R.S., F.G.S., &e.

[Puartes I., IL., I1T.]

ContTENTS.

Dioritic Rocks.

Introduction. 5.
6. Upper Oolitic Series with inter
Ue
8.

. Tertiary and Diluvial Formations
- of the Coast.
. Saline Formations.
. Diluvial Formations of the Inte-
rior.
. Voleanic Rocks.

—

stratified Porphyritic Rocks.
Permian or Triassic Formation.
Carboniferous Formation.

Co bo

9. Devonian Formation.
10. Silurian Formation.

e

Introduction.—In laying before the Society a statement of the ob-
servations made during an examination of Peru and Bolivia, in the
years 1857, 1858, 1859, and 1860. I may observe that the present
memoir is to be considered as the first part of a report of the results
obtained during my travels in South America during these years ;
and, consequently, it is believed that the conclusions here arrived at
will have more weight when considered in conjunction with the ob-
servations on the geology and mineralogy of the neighbouring re-
publics of Chile and the Argentine provinces, which subsequently I
shall have the honour to lay before the Society,—more particularly
as several of the geological formations not well developed or examined
into in the district forming the subject of this memoir exhibit them-
_ selves much more characteristically further south.

Many points will be found not so elucidated or examined into as
could be desired, and might appear to have been neglected; this,
however, has not arisen from oversight, but is due to the great dif-
ficulties and frequently severe privations encountered in exploring a
country in many parts entirely uninhabited or in next to a savage
condition, and further by my haying been limited as to time and
pecuniary resources, and hampered by other occupations and by the
political state of the country.

In the construction of the accompanying Map and Sections (Plates
I. & I1.), Nos. 1 & 2 of which give a good idea of the structure and
formation of the different mountain-ranges of the Andes, the hori-
zontal distances are laid down from the best local information which
could be procured, and from data furnished by the Bolivian Govern-
ment-survey lately completed. For the vertical altitudes in addi-
tion to those determined by myself barometrically, and occasionally
by boiling-point and trigonometrical observations, I have employed
some of the heights noted on Mr. Pentland’s map,—and further the

8 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

following series of observations made by a gentleman for some time
my fellow-traveller, Captain Friesach, of the Austrian army, as given
in the annexed Table.

Elevation Elevation

Tocality. aor Locality. pene
feet. || feet.

ATCA Reset cae ne catenin ashes 20 | La Paz (highest part) ...... 12,270
acne tation ketene cet eee 1,950 || La Paz (Ajiameda)............ 11,980
IDach iawn, (onetes scone SOO} || Mallocaton sseceseeeceee eee 8,150
Palcatsass. Sts cacseteeee 9'700" |" Cotanax <5 ceeoeeeeeeeeee 7,990
lay] Raya IGVe eS ee sonoonaosccooe 12,630 | Hacienda de Illimani ...... 10,010
Alto de Guaylillos............ WA}G50) || Santiacon.-..-..-ss-e soe ceee 8,940
PAN CATA'-Tacesncccoacceseentessese 13,750 |, Rio de la Paz on entering 3.380

iWehusumaeesese seen eceeee ISHN) |) GRIER) posca Encscoccooss :
Liao) AY NTE ooaoprooposdocacsedne 13,560 | Rio de la Paz below Toca...) 4,204
Pailumani ........ Se: AM 14725) | Norpana.,-.sce-ecccee sass 6,870
Chulluncayani (pass) ...... 13,680 | River below Yrupana ...... 4,570
Santiago de Machaca......... 1277/70) |\'Culumaniy i. -.--cctesceeesesee 6,460
San Andres de Machaca_ ..| 12,890 | Rio de Tanampayo ......... 4,320
INasacara) “.cccsesesscwasreaese 12710) |) Coripata,.2....-2-eas-reteeees 6,360
SUTITOsse case he cone VWB56D | Corieco sc. s2-aseecesaeeareee eee 6,530
Pacheta del Rio Colorado...) 14,210 } River near Corioco ......... 3,925
Conim brah Pee eee, | 12,950) || Sandillan’ .....2..0..2.csesees 7,040
Biacha te 2655.2staeecsesespones 12780 | Highest point Toate f 11.830

(indiayi\y. -so0 sasesesseeaks. | 10,780 Sandillan and Unduavyi 4
Highest points Pea) 15.630 | Copacabana ............0.+0+- 12,730
Unduavi and La Paz... [| ~??”" Puno(shoreof LakeTiticaca)| 12,630
Tambillo de Laja ............ | 12,830 || Ariquipa (plaza)*............ 8,840
DisarnaderOlss.estses-eeen ee | 12.680 | Summit of Misti, or vol- \ 19.876

Altoide Potosi: c.......+-te- | 13,580 cano of Ariquipa*...... 3

* The height of the plaza of Ariquipa was determined by the Torricellian
| experiment, and found as stated above; the summit of Misti or volcano of
| Ariquipa was found to be 11,456 feet above the plaza bya trigonometrical

| measurement.
|

And lastly, in addition to these, the following Table of heights of
mountains in English feet has been calculated from some of the
results obtained by the recent Government-survey of Bolivia.

Elevation Elevation
Mountain. ae anelich Mountain. aealich
feet. feet.

WEN TRyS YH nasBhacaadetassasnesene PA 812)|)"Mornratea .222-<25 se eee 20,418
UR ian tse seta. sree ees 2A NOD || Callinsant 22. .cs-pe.ce-seeeccre 20,530
Sajama (volcano) ............ 23014." || Potosi! 277525 eee 15,724
Coololo (Apolobamba) ...... 22,374 | Tunari de Cochabamba...... 15,608
Hua yna Bolost esas; <402- 21,882 | Hermoso de Aullagas ...... 15,747
Cachacomani (voleano)...... 21,583 || Portugalete ............0-.-+ 14,720
Quenuata f peaks of Tacora) 21,252 || Espejos .................se0e+ 9,337

| Chipicani) _—_(voleano) 22,687 | Misti (volcano of Ariquipa)| 20,150
|

1860. | FORBES—BOLIVIA AND PERU. 9

The strike and dip of the rocks, when not otherwise stated, are
given with reference to the magnetic meridian.

In the arrangement of my notes it was found most satisfactory to
classify them according to the geological age of the deposits in ques-
tion, commencing with the most recent.

1. Tertiary and Diluwial Formations of the Coast.—The older
Tertiary beds of shells so characteristic of many parts of the Chilian
line of coast do not appear to present themselves from Mexillones
northward to Arica; but we find at intervals shell-beds, containing
exclusively shells of species now inhabiting these waters, elevated to
a small height above the sea: I did not, however, observe any beds
reaching an elevation of 40 feet above the present sea-level; and
although the whole line of coast shows unquestionable signs of re-
cent elevation, still the evidence is not so satisfactory, and appears
to point cut a much more irregular action than further south along
the Chilian coast-line.

- At Cobija 1 discovered a bed of shells in the immediate neigh-

bourhood, to the south of the port, about 25 feet above the present
sea-level; and, on examination, this was found to contain only species
at present inhabiting these waters. Among these shells I recog-
nized the following genera :—

Concholepas. Fusus. Patella.

Mactra. Oliva. Fissurella (2 species).
Venus (2 species). Trochus. Chiton.

Mytilus. Turbo. Serpula.

Tellina. Turritella. Balanus.

I found also fragments of an Echinus and bones of a Seal. Whilst
digging in this bed, I came upon a small piece of wood in a decayed
state, which evidently had been shaped by human hands, and bore
marks of having been cut by a sharp tool, most likely of steel, as
some of the cuts appeared much too defined to be attributed to a
stone or other dull instrument.

On the rocks close to the town are some deposits of guano, which
are being worked to advantage, although in quality and thickness
much inferior to the guano from the Chinchas Islands pertaining to
Peru. These deposits are situated at from 20 to 40 feet above the
sea-level, and in appearance are very similar to the Chinchas beds
on a small scale.

On the surface of these deposits, and also between the beds of the
same, my attention was attracted by a crust or bed of a harder sub-
stance, of a light-brown colour, varying in thickness from a few
inches to one or more feet, and possessing a semicrystalline and
rather saline appearance, with occasionally a faint ammoniacal odour.
On examination I found it to contain a large amount of ammonia
in a state of combination ; and, at the request of the Bolivian Go-
vernment, it was analysed by Mr. Francis Ignacio Rickard, of Val-
paraiso, who obtained the following per centage composition :—

10 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

Waterss: et TON, ch Ay An ae ee 12-45
Organie matter el. kee eee 17°48
Chiondetofammonium) =. eee eee 30°20
Phosphate! of linte se) Rae ee eens 10-00
Sulphaterotlime 2. eee ee 0-80
Chiorndeyohsodium= sens. eee 16-03
ROH OCGL SCC RCSA MMM deri te oc UEC a a ea 3 Es ae 1-60

98:56

From the above results it is evident that this substance had been
produced by the action of sea-water, probably thrown up in the form
of spray, on the guano-beds. The amount of ammonia contained in
this material being much greater than in the unaltered guano itself,
this substance, formerly thrown aside as worthless, is now exported
in large quantities, under the name of “ Huano petrificado,” realizing
a price considerably higher than the guano with which it occurs.
The low elevation of these guano-deposits above the present sea-level, _
and their thickness, which is frequently not less than 10 to 15 feet,
sufficiently prove that, in parts at least, they are of later origin than
the shell-beds previously described. Other similar guano-deposits
are met with at Mexillones, Algodon Bay, the newly discovered San
Felipe Islands, and at various parts along the coast.

At several places along the coast the raised beaches are strongly
impregnated with salt, which occurs both in the form of small layers,
or imbedded, as well as irregularly distributed in the diluvial detritus.
This is the case at Molle, Ceremono, and Patillos, all to the south of
Iquique, and several other places. These saline deposits are found
at the height of from 10 to 40 feet above the present sea-level ; at
the two first-mentioned places the salt is so abundant that cargoes
have occasionally been-shipped from them. On the top of the Morro
de Arica, a hill about 500 feet above the sea, small superficial layers
of tolerably pure salt, from 3 in. to 3 inches in thickness, are also
met with ; and the fissures on the side of the same hill are often found
to be filled with veins of salt.

At Arica I was not successful in finding Balani and Millepore
attached to the sides of the “‘ Morro”? hill, as described by Lieutenant
Freyer* ; and the many loose sea-shells met with on the sides and
summit of the same I believe to have been brought there by the nu-
merous sea-birds, probably assisted, on the south slope, by the action
of the winds and shifting sands,

That no very perceptible elevation has taken place in the imme-
diate neighbourhood of the Morro of Arica (or, if such an elevation
had taken place, that it has been followed by a subsequent depression
to nearly the same level) during the last 350 years, or since the
Spanish conquest, appears from the numerous Indian tumuli found
along the beach, for miles south of the Morro; many of these are not
20 feet, and some probably considerably less, above the present
sea-level. That these tumuli have not been constructed since the

* Darwin’s ‘ Geology of South America,’ p. 47.

1860. | FORBES—BOLIVIA AND PERU. 1

Spanish invasion may be inferred from the ornaments of gold found
in. them, along with the mummies, one of which I was informed had
been found by Mr Evans, the Engineer of the Arica and Tacna rail-
road, enveloped in a thin sheet of gold.

Along the Coast of Chile, on the contrary, there is the fullest evi-
dence to prove that, since the arrival of the Spaniards, a very consi-
derable elevation of the land has taken place, over the greater part,
if not the whole extent, of the line of coast.

North of Arica, if we accept the evidence of M. @ Orbigny and
others, the proof of elevation is much more decided ; and consequently
it may be possible that here, as is the case about Lima, according to
Darwin, the elevation may have have taken place irregularly in places;
but at the same time a depression or submergence, as at Callao, could
hardly have taken place without haying destroyed these Indian tu-
muli, formed in the loose sand, and quite incapable of resisting the
action of the waves, which produce a strong surf along this rugged
coast.

With regard to the evidence of the rise of the land, deduced from
the occurrence of sea-shells strewed over the surface of the higher
ground further inland, it must be remembered that the numerous sea-
birds which feed on shell-fish frequently carry their food to consi-
derable distances from the sea, and likewise that shells are occasionally
transported inland along with the sand in the shifting sand-dunes
which are common enough along the coast ; where the slope is gentle,
as in the immense inclined plains to the north of Arica, this may fre-
quently be the case. These sand-dunes appear to attain their great-
est mobility during the hot season, when the parched sand rolls
along impelled by the slightest breath of wind, and several times re-
minded me of the extraordinary mobility presented by silica and some
other substances in a state of fine division when heated in a crucible
or other vessel, especially if, as 1t were, provoked by the slightest
touch of a rod.

An observer, travelling quickly over the ground, might easily be
deceived, and regard as evidence of elevation the occurrence at some
few spots of innumerable shells spread over a small area or patch in
the midst of this desert landscape. On examination, these are found
to be a land-shell (a species of Bulimus) about 3 to 1 inch in length ;
and it is difficult to account for their presence in these spots, desti-
tute of all vegetation, except on the supposition that they have made
their appearance thus abundantly in years favoured with some showers
of rain, whick may have developed in these scattered spots a vegetation
sufficient for their sustenance. I have noticed the occurrence of such
spots covered with these shells in the midst of these desert-tracts,
down to as far south as Choros Bajo, a little north of Coquimbo in
Chile. Professor Philippi has also observed them at the Morro de
Mexillones.

The coast from Mexillones to Arica is formed by a nearly con-
tinuous chain of mountains, rising abruptly from the water’s edge,
and attaining an average elevation of about 3000 feet, but diminishing
in height towards their northern limit, the Morro of Arica, which

12 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

does not exceed 600 feet above the level of the sea. An occasional
narrow strip of sea-beach is seen bordering this range, and is com-
posed exclusively of the débris of the mountains themselves, which,
being in many places nearly perpendicular, expose to the spectator,
passing along in the coast-steamers, a fine section of the shales,
claystones, and imbedded porphyries which here represent the Upper
Oolitic series, and are occasionally seen disturbed and altered by the
intrusion of dioritic rocks of a later age.

At Arica, however, this range of mountains suddenly recedes from
the coast, leaving an saircramn cc na space, about 30 miles broad and
extending as far northward as examined, occupied by gently sloping
plains, evidently ancient sea-beaches, which rise to the height of
about two thousand feet above the sea-level. These plains, being
for the most part entirely destitute of water (as no rain falls in these
regions), are consequently entirely barren, and present to the eye of
the traveller a most desolate and arid appearance. When, however,
as in the valleys of Tacna, Sama, and Azapa, a scanty supply of
water does occur, the soil, noted for its surprising fertility, produces
a most luxuriant vegetation of a semi-tropical character.

These plains are composed of sand, earth, and gravel, with abun-
dant fragments, more or less rounded, of the porphyritic, dioritic,
and volcanic rocks forming the coast-range of mountains which
bound them to the eastward. Even after a most careful examination,
no single fragment or boulder of any extraneous rock was met with ;
so that no drift-action appears to have assisted in the formation of
these beaches, which appear due solely to the action of the waves
beating against the former rugged line of coast.

In the Sections No. 1 and 2, Pl. I1., which cut through this district,
it will be observed that a volcanic formation, apparently contempora-
neous, is situated in the midst of these plains, which does not bear
the appearance of having been injected into the diluvial beds forming
them, but rather to have flowed over them, or more probably to have
been deposited on the top of them whilst still under water, in the
form of a tuff or volcanic ash, and subsequently to have again been
covered up by similar diluvial matter; a more detailed examination,
however, is necessary to settle the question. I may mention that
Dr. Vance of Tacna informed me that near the railway at that place
the ground in a cutting was found to be burnt and altered, as if by
igneous action; this appears to me as more probably due to still
later volcanic activity.

The rocks of this voleanic formation are all trachytic, and fre-
quently present a most striking similarity to the domite of Auvergne,
being, like that, composed of quartz, black or brown hexagonal mica,
and a weathered-looking felspar, and form some four or six beds,
superposed one on another, and of an average thickness of about 10
feet each; these are either a white trachytic tuff, like domite, with
abundant imbedded fragments of pumice, or a compact trachyte of a
reddish or white colour and similar composition.

These trachytic tuffs form an excellent building-material, from the
ease With which they are worked and shaped, and are very exten-

1860. | FORBES—BOLIVIA AND PERU. 13

sively employed for this purpose at Arica and Tacna. In the quarries
of this rock near Tacna I discovered a mineral very much resembling
allophane in external characters, but differing in only containing
28-49 per cent. of water: it occurs in fissures in the trachytes,
forming veins of from a line up to some inches in thickness, and is
probably derived from the decomposition of the felspathic element of
the trachyte by the action of water.

2. Saline Formations.—Later in age than the Tertiary deposits,
the saline formations so characteristic of this part of South America
are not, as frequently supposed, merely confined to the country
surrounding the port of Iquique, but appear at intervals scattered
over the whole of that portion of the western coast on which no rain
falls, extending further north than the limits of the map accompany-
ing this memoir; whilst to the south they run entirely through the
desert of Atacama, and even show signs of their existence further
south than Copiapo in Chile, thus stretching more than 550 miles
north and south; their greatest development appears, however.
between latitudes 19° and 25° §.

They are generally superficial, but occasionally reach to some
small depth below the surface, and then may be entirely covered
over by diluvial detritus ; they always, however, show signs of their
existence by the saline efflorescence seen on the surface of the ground,
which often covers vast plains as a white crystalline incrustation, the
dust from which, entering the nostrils and mouth of the traveller,
causes much annoyance, whilst at the same time the eyes are
equally suffering from the intensely brilliant reflection of the rays of
a tropical sun.

The salts forming these “ Salinas,” as they are generally termed,
are combinations of the alkaline and earthy bases soda, lime, mag-
nesia, and alumina, with hydrochloric, sulphuric, nitric, and carbonic
acids, and occasionally with boracic, hydriodic, and hydrobromic
acids,—and in combination present themselves as the following
minerals in a more or less pure state:—Common salt, epsom-salt,
elauber-salt, thenordite, glauberite, soda-alum, magnesia-alum, gyp-
sum, anhydrite, along with chloride of calcium, iodide and bromide
of sodium, carbonate and nitrate of soda, and in some places borate
of lime and borax.

With the exception of the boracic acid compounds, the presence of
which (as subsequently will be attempted to be proved) is due to
volcanic causes, all the mineral substances found in these “ Salinas ”
are such as would be left on evaporating sea-water, or by the mutual
reactions of the saline matter thus left on evaporation on the lime,
alumina, and organic matter found in the adjacent rocks, soil, and
shell-beds; and as we have indisputable evidence of the recent
elevation of the whole of this coast, and bearing in mind likewise
that no rain falls in these regions, it appears very reasonable to
suppose that all these saline deposits owe their origin to lagoons of
salt water, the communication of which with the sea has been cut
off by the rising of the land. When studying the structure of the
mountain-ranges near the coast, it was also observed that, at all the

14 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

large saline deposits, the chain of hills to the westward or sea side of
the “Salinas” is of such a formation as might on elevation be ex-
pected to enclose a series of lagoons, which, by means of the breaks
or lateral openings in the chain itself, could for a longer or shorter
period keep up a tidal or occasional communication with the sea when
high, which thus would pour in a fresh supply of salt water to make
up for the loss sustained in the lagoons from the evaporation produced
by the heat ofa tropical sun. It is therefore not necessary to suppose
that the great amount of saline matter generally present in these
deposits is due to the salts contained in an amount of sea-water
merely equal to the quantity originally contained in the lagoon, or,
in other words, to the cubical contents of the lagoons themselves.

The occurrence of salt at different places along the coast at very
small elevations above the sea, previously noticed, is no doubt due
merely to the tidal infiltration of sea-water into the porous shingle
and other beds, and its subsequent evaporation; and must not be
confounded with the much greater and more elevated saline deposits
further inland, which are met with at three very different altitudes
above the sea, as follows :—

(1) At, approximately, from 2500 to 3500 feet,

(2) ” 7000 to 8000 feet,
(3) 3 12,500 feet

above the present sea-level, and which appear to indicate three di-
stinct and important changes in level in this part of South America.

(1.) The deposits situated at about 2500 to 3500 feet above the
present sea-level include the important beds of nitrate of soda so
extensively worked along this coast, and appear to run from latitude
19° southward into the northern part of the Desert of Atacama,
showing themselves, according to the configuration of the country,
at distances varying from 10 to 40 miles inland.

When in this part of the country, I had not time to make a more
detailed examination of these saline deposits than was necessary to
enable me to arrive at a conclusion as to their mode of formation and
the origin of the nitrate of soda contained in them.

All the data that I could obtain appeared fully to confirm the “la-
goon hypothesis” previously mentioned, and to prove that the ori-
ginal constituents of these beds had merely been such salts as would
result from the evaporation of sea-water. The nitrate of soda and
some other associated compounds are due to subsequent reactions,
and consequent decomposition of the salt of the original deposit,
mainly produced by the agency of carbonate of lime and decomposing
vegetable matter.

The first step in the formation of nitrate of soda appears to be the
decomposition of the chloride of sodium, or salt, by carbonate of lime
(in the form of shell-sand, &c.) with the production of chloride of
calcium and carbonate of soda, both of which salts have been shown
to be present in quantity in the soil of these nitrate-grounds.

The carbonate of soda thus eliminated, when in contact with the
mixture of shell-sand and decomposing vegetable matter which may

pe

1860. | FORBES—BOLIVIA AND PERU. 15

be expected to result from the luxuriant vegetation around such a
tropical swamp, and from the abundant marine plants in the lagoon
itself, would realize the conditions of the French artificial nitre-beds,
substituting only carbonate of soda for the carbonate of potash there
used: we may consequently, with all fairness, expect a similar result
in the production of nitrate of soda on a still larger scale.

This view appears much strengthened by the occurrence of wood,
reeds, or rushes, and other vegetable matter in the nitre-grounds at
but little below the surface, as well as from the general position of
the nitrate of soda in the saline deposit, as it invariably occurs in
the margin or outer edge of these, representing the shelving sides of
the hollow or lagoon-basin, the central part of which is composed of
layers of sea-salt only, frequently several feet in thickness.

In seeking for nitrate of soda, the searchers always look to the
rising edge of such salt-basins, and further judge of the probability
of finding the nitrate from a peculiar moist or clammy state of the
ground, which is due to the presence of the chloride of calcium pro-
duced by the decomposition above explained.

The quantity of sulphates, and more especially of sulphate of lime,
included invariably in these deposits might, at first sight, appear to
the observer too great to suppose it due only to the evaporation of
the sea-water; but I believe that this impression will be dissipated
when he sees the enormous amount of gypsum removed in the form
of hard white cakes, or sedimentary crust, from the boilers of the
large distilling machines in use along this arid coast for producing
from the water of the sea a supply of fresh water for the main-
tenance of the inhabitants, beasts of burden, and even the locomotive
engines of the railways along this coast. It appears not necessary
to suppose, as has been put forth, that the sulphates present have
been formed by volcanic exhalations acting upon the beds of salt.
The boracic acid compounds met with appear, however, to be due to
this cause; and the borate of lime met with in such large quantities
appears to be indirectly produced by the condensed vapours of
volcanic fumeroles, many of which are still in full activity in this
district.

The gaseous exhalations of these fumeroles have, I believe, never
been submitted to a chemical examination ; so that the presence of
boracic acid has not actually been proved; it may, however, be in-
ferred from the general resemblance which these fumeroles bear to
those of Tuscany, the Lipari Islands, &c., where it is known to exist.

The borate of lime is found only on the more elevated part of
this saline district, occurring on the eastern side of the same, where
the rising ground begins to form the western slope of the adjacent
cordilleras.

As voleanic action is developed on a grand scale in this moun-
tain-range, such solfataras or fumeroles, forming lateral orifices on
the side of the mountains, are very common; and we may expect that
the waters coming down this slope carry with them in solution the
boracic acid contained in the condensed vapours of these solfataras,
which, coming into contact with the lime of decomposed porphyry-

2

16 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

rocks, or the shell-sands of the plains below, would combine readily
to form the nodules of borate of lime here met with.

It has been suggested that the nitrate of soda likewise owes
its origin to similar causes; I consider, however, this view to be
untenable where the vapours themselves, from the great amount
of sulphurous and hydrosulphurie acid gases which they contain,
are of so eminently deoxidizing a nature as to decompose any
nitric fumes evolved by such volcanic action. I therefore believe
the nitrate of soda wholly due to the chemical action previously ex-
pounded.

The saline deposits of this series do not rest directly on the
rock itself, but on a beach more or less level, or hollowed out into
lagoon-basins, and composed, as the present and the raised sea-beach
previously described, of the débris of the adjacent porphyritic, dioritic,
and voleanic rocks.

The deposits explored for nitrate extend from the river of Pisagua
southward to Patillos, a distance of about 110 miles; but latterly
new and extensive deposits have also been worked further south,
inland from Tocopilla. There is, however, no doubt that they exist
along the whole coast-line depicted on the accompanying map, at
from 10 to 50 miles inland; the borate deposits, however, appear to
recede from the coast, as they occur more to the south, and strike
to the eastward, following the line of volcanic action, mdicating
thereby their connexion with the same.

(2.) The series of saline deposits next in elevation are situated
at from 7000 to 8000 feet above the level of the sea, and are de-
veloped on a grand scale in the northern part of the desert of
Atacama,—the great “ Salina de Atacama” extending 100 miles or
more from S.E. to N.W., with a breadth of 20 to 30 miles, and
the lesser “‘ Salina de Punta Negro” still further south (about 30
miles long and 12 broad)—two examples of immense salt-plains,
apparently resulting from the drying up of such lagoons as those
before described.

Not having made a personal examination of these, I am not ina
position to give any detailed account of them; in fact, they are only
known in name and extent, and have never been examined.

(3.) At an altitude of about 13,000 feet above the sea, saline matter
is found to occur in a manner similar to that of the last-mentioned
deposits. In Section No. 2 (Pl. II.), at ‘‘ Laguna Blanca,” extensive
plains and salt-lagoons are found,—the latter still existing as lagoons,
since they are now situated on the extreme borders of the rainless
region, whereby the loss from evaporation is supplied, in part, by the
rain which falls ; and thus we generally find extensive plains covered
by white crystalline salt, forming the circumference of some small and
generally shallow lake, deserving only the name of a swamp except
in the rainy season of the year. This saline formation, I believe, is
seen more or less developed all the way to Oruro, and thence over the
saline plains of Sora-Sora, it extends much further south, but, like
the last, has not as yet formed a subject for more minute examina-
tion, and, from its occurring in districts exposed to a heavy annual

1860. } FORBES—BOLIVIA AND PERU. 17

fall of rain, is naturally not so characteristic in its development as
the two previously described formations, although at the same time
it presents some very striking features, and in some respects strikingly
reminds us of its supposed lagoon origin.

3. Diluial Formations of the Interior.—The saline deposits last
noticed are situated in the midst of what may be termed the great
Bolivian plateau, having an average altitude of fully 13,000 feet
above the sea, and bo unded to the west by the Upper Oolitic rocks
of the coast- cordilleras, whilst to the east it abuts against the Si-
lurian range of the true Andes. This plateau is not ‘uniform in its
mineralogical nature; and when viewed in section from east to
west, it shows considcrabie diversity of composition, arising from
the ranges of hills which intersect it all bearing ‘nearly north and
south, and thus dividing it into so many longitudinal valleys (see
- Pl, I).

These valleys are generally occupied by nearly level plains, formed
of the gravelly spoil } produced by the wearing down of the bounding
ridges, with which they are consequently identical in lithological
composition. The ridges themselves seldom attain a greater eleva-
tion than 2500 feet above the plateau, and are generally under this
height ; but occasionally volcanic cones thrust themselves up to more
than 6000 feet above the plain, and consequently attain an eleva-
tion of fully 20,000 feet above the sea-level.

The character of this plateau is well shown in the Sections Nos. 1
and 2 (Pl. I1.), by a reference to which it will be seen that it may be
separated into three divisions—western, central, and eastern (Oolitic,
Permian, and Silurian, according to the nature of the rocks origina-
ting the diluvial accumulations which fill up the intermediate basins
or valleys).

The most western of these is essentially composed of Upper Oolitic
detritus, with an occasional block of diorite, and in places abundant
volcanic débris from the neighbouring eruptions. They are covered
with but a very scanty verdure, if not entirely barren, and incrusted
with saline matter, and are generally either entirely destitute of
water, or possess some few springs at great distances from one
another and of abominable quality—frequently, as at Rio de Azufre
(Section No. 2), not potable, and even causing death to the animals
which drink it, as sufficiently proved by the bones of mules, llamas,
&e., scattered along the banks. At most places the water generally
produces bad effects to those unaccustomed to it, even when it is
comparatively tasteless.

From an examination of the waters from several localities, I may
observe that in one or two cases it was perfectly astonishing what an
amount of saline matter might be present in water which might be
termed “ palatable,” but which produced strong purgative effects ;
on examination, such a water from the desert of Atacama was found
to contain a very large amount of the sulphates of soda and mag-
nesia (Glauber and Epsom salts), associated with common salt and
carbonate and sulphate of lime; and I can only suppose that the
bitter taste which the amount of sulphate of magnesia (Epsom salts)

VOL. XVII.—PART I. c

18 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

present would alone produce had been neutralized or concealed by
the admixture of the other salts.

In the midst of these plains at Ancara, I noticed some recent con-
glomerate-beds, of a brown colcur, composed of small and very angu-
lar pebbles, and more hke a breccia than a true conglomerate. They
were of very small extent, and had an apparent strike nearly N. and
S., with a low dip to eastward.

The central division of this diluvial formation is distinguished at
first sight from either of the others by the redness and sandy nature
of its soil, showing at once its derivation from the Permian or Tri-
assic sandstones and marls; occasional patches are eovered by vol-
canic detritus where the sandstone hills have been disturbed by the
intrusion of the trachytic rocks, well illustrated m Section No. 1.
The plains thus formed are well watered and frequently marshy,
and are cut up by numerous rivers, at least in the northern part
of the district here described*; we do not find the surface-water
saline, as is invariably the case in the western division ; bet occasion-
ally, as for example at Santiage and at San Andres (both on Section
No. 2), we meet with brine-springs, which furnish the inhabitants
with an abundant and cheap supply of culinary salt of excellent
quality, by simply allowing the water to evaporate in the open
air from the heat of the sun. These brine-springs are most pro-
bably due to salt-beds situated at greater depths im the sandstones
of the formation itself, and not to be attributed to saline deposits of
more recent origin.

The third or eastern division of this plateau is, in its turn, so dif-
ferent in character from either of the preceding, that it is at once
recognized when encountered.

In Sections Nos. 1 and 2 (Pl. II.), this formation is seen as a
great plain abutting to the east against the Silurian rocks of the
highest range of the Andes, to the débris of which it owes its origi ;
whilst to the westward it is confined by the range of low hills of
Devonian strata which separate it from the central division of this
diluvial formation. The intermediate basin, occupying the space be-
tween these Silurian mountains and Devonian hills, is filled up to the
level of the plain by an immense accumulation of clays and gravels,
with larger pebbles and boulders of Silurian and granitic rocks,—the
former being represented by grauwackes, indurated sandstones, clay-
slates, and shales, which latter occasionally contain fossils of Silurian
age.

Where, as in the valley of the river of La Paz (which from its
abruptness might almost be termed a ravine), a section of this basin
is disclosed (Section No. 2), its surprising magnitude is seen, as in
this place. The thickness, reckoning from the level of the plain

* I may here mention that m a spring at Comanche, the water of which
appeared to feel slightly warm on immersing the hand, I found numbers of a
small univalve shell; and on submitting them to the inspection of Professor
Philippi, of the University of Santiago, in Chile, he considered them identical
with his Paludina Atacamensis, which he discovered in a tolerably hot spring at
Tilopozo, in the northern part of the Desert of Atacama.

1860. ] - FORBES—BOLIVIA AND PERU. 19

above down to the Alameda of La Paz, was found by measurement
to be 1650 feet, consisting of alternating beds of grey, bluish, and
fawn-coloured clays, gravel, and shingle-beds, along with boulders of
clay-slate, grauwacke, and granite, frequently of enormous size, and
well rounded as if by the action of water; the beds are nearly hori-
zontal, or dip to the south. About 300 feet below the surface of the
plain, there is seen in this section a bed of trachytic tuff, evidently
volcanic, and about 20 to 30 feet in thickness. This is visible at a
great distance as a white band, running along the precipices encir-
cling this valley or ravine, and appears to be contemporaneous with
the beds of clay, gravel, and boulders, which, with this solitary
exception, form the rest of this diluvial accumulation, and which,
except in the uppermost beds, do not contain, as far as I examined,
any volcanic detritus.

No trace whatever of volcanic activity being found anywhere in
the neighbourhood of La Paz, I was for a long time greatly puzzled
to account for the occurrence of this very peculiar bed in the midst
of diluvial strata. The general inclination of the beds themselves,
dipping to the south, indicated that they had been drifted from the
north or north-east, and they appeared to become narrower towards
Lake Titicaca, near which I found the large volcanic outburst of
trachytic and trachydoleritic rocks shown in Section No. 1, and from
which doubtless the tuff forming these beds had emanated, and had
been carried down by aqueous action, and deposited as a sedimentary
bed in the series of clays, gravel, &c., forming this great thickness
of drift.

The total thickness of these beds below La Paz must certainly
exceed 2000 feet, and probably reaches 2500 feet, being certainly
one of the most finely developed examples of this class of deposit,
both as to magnitude and superficial area. I am unable to assign
any correct limits to this formation, which appears to extend from
north to south through the entire length of Bolivia; to the north,
or towards the Lake of Titicaca, it appears to diminish in thickness,
and may possibly wedge out entirely. The beds seem to have a
general, but slight, dip to the southward.

I may here mention that in a small pool of water at a place called
the Tambo de Perez, about half-way between La Paz and the Lake
of Titicaca, I found numbers of a small fresh-water bivalve, which
Professor Philippi, of the University of Santiago in Chile, kindly
examined for me, and pronounces to be the Cyclas Chilensis
(D’Orbigny), found first near Conception in the south of Chile,
where it is common, according to Dr. Philippi, both in Valdivia
and Puerto Montt. In these localities this shell is found at but a
small elevation above the sea-level, in the coldest inhabited part of
Chile ; whereas in Bolivia, as above stated, we find it under the tro-
pics, but at an elevation of about 14,000 feet above the sea; so that,
we may here regard this excess in elevation above the sea-level as
equivalent to the difference of about 40 degrees in latitude.

Amongst the clay-beds of this diluvial formation, near La Paz, as
also at the foot of [mani and near. Poto-Poto in the valley of the

C2

20 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

River Chuquiaguillo, I found interstratified a bed of carbonaceous
matter, approaching to lignite. In many parts this appeared as if
wholly composed of carbonized marine or marsh plants, resembling
rushes, reeds, and alge; but I likewise found one or two pieces of
unmistakeable lignite or carbonized wood. At all these places it is,
probably, that it is but one and the same bed which appears at Poto
Poto; this bed does not attain a thickness of more than from 6
inches to a foot. At the foot of Illmani it is, however, of much
greater thickness.

A chemical examination, which I made of several of the clays from
these strata near La Paz, showed that they contained but a mere
trace of lime, as might be expected, knowing that the Silurian rocks
of the high Andes, from which they appear to have been derived,
contain but traces of limestone.

As the Silurian origin might indicate, this formation is everywhere
eminently auriferous, and has been both since, and probably even
before, the time of the Incas very largely explored for gold. The
great quantities of gold found in Peru at the time of the Spanish con-
quest, had in greater part, if not wholly, been derived from these
diluvial accumulations.

The rabbit-like burrows made by the Indian gold-workers into
the more auriferous beds are everywhere visible along the sides of
those valleys where a supply of water was not too distant to prevent
these workers from transporting the auriferous earth for the purpose
of working it: and frequently later explorations have disclosed the
mummies or skeletons of unfortunate Indians, who have perished in
these narrow and tortuous holes, from the falling in of the superin-
cumbent earth, and been buried along with their mining implements.

This system of working is now entirely abandoned, and the mode
of operating is very different at present, and can easily be understood
from the annexed sketch (fig. 1), which may be supposed to repre-
sent a general view or sketch-section of the operations carried on at
the gold-washings of Chuquiaguillo, near La Paz, belonging to Mr.
Saienz of that city.

As will be seen in this sketch, the valley is, in the first instance,
completely closed up, and the course of the river stopped, by a rude
wall or dam of stones and earth, provided with sluices, and having
a portion of the wall seen to the right hand somewhat lower, in order
to carry off any overflow of water which otherwise might disturb the
workings. A longitudinal excavation is then made close up to the
one side of the valley, and of such breadth as can be conveniently
carried on by the number of hands at disposal ; and,in making this,
the large boulders and stones, too heavy to be carried off by the rush
of water, are piled up to one side, whilst the earth, gravel, and clay
are merely loosened and flushed off by the water turned on from the
sluices, allowing the force of the stream to car ry them down the river.
On arriving at the several successive auriferous beds, which are
known from previous trials, and which are denoted by the dark
bands running horizontally across the excavation, as seen in the sketch,
more care is taken, but the whole of the auriferous earth is likewise

1860. | FORBES—BOLIVIA AND PERU. 21

flushed off, and, being so much heavier than the rest, deposits itself
at but a little distance from the workings, where it is collected and
subjected to repeated washing in a trough until nothing but the
gold-dust remains behind.

Fig. 1.—Sketch of the Gold-washings on the River Chuquiaguillo.

A Eira b aid f ; Ae
A AC ea a | TS a ey
. ie gees ar” a

“I

This excavation 1s deepened until the lowest available auriferous
stratum has been reached, and then abandoned, in order to carry on
the same operation parallel to it; the boulders and stones met with
in the new working are thrown into the old excavation, and such
excavations are continued right across the valley. In a valley of
considerable breadth it would be impossible, except by employing an
immense number of hands, to open out and lay bare the whole of the
auriferous ground in one excavation.

The auriferous strata occurring in these diluvial accumulations
are, in Bolivia, generally known by the name of “ Veneros,” and ap-
pear to correspond to what are technically termed ‘“ floors ” by the
gold-diggers of California and Australia, being, as it were, the floor
or clay-bottom upon which the gold-dust had settled down, subse-
quently covered up by alternating beds of coarser sand, gravel, and
boulders: above this a similar floor and coarser beds might in their
turn be found, as in the sketch of the washings on the Chuquia-
guillo (fig. 1): and where these diluvial strata are of still greater
thickness, a proportionate number of “‘ veneros ” are generally found
to occur.

These ‘ diggings” are, as might be expected, confined to the sides
of valleys and beds of rivers which contain water* sufficient for
washing. The celebrated workings of Tipuani and those in the

* The rivers of this part of the world are too frequently ‘‘ Rios Secos,” a
Spanish term which is generally adopted.

22 PROCEEDINGS OF THE GEOLOGICAL society. __[ Noy. 21,

Yungas appear also to belong to diluvial accumulations of this same
geological age.

The valley of La Paz, being entirely cut out of this great diluvial
formation by the action of the river which traverses it, is, as might
be expected, often exposed to considerable landslips during the
extremely heavy rains of the wet season: when residing there, I
witnessed such a landslip, which blocked up the valley and caused
it to be inundated to a considerable distance by the damming up
of the river. In many parts also the action of the rains and small
rivulets formed by them, cutting through these immense clay and
gravel strata, forms a most striking and picturesque landscape.
The slope of the valley of La Paz, for example, is seen cut up into
innumerable ravines of great depth, whilst pinnacles of more than
60 feet in height will be left standing in great numbers and of all
variety of form, frequently quite isolated, and, from their slender
proportions, often looking like needles or pillars formed artificially :
the sides of these show a very pretty section of the variegated clays
and gravels that previously had formed the beds from which these
had been carved out and left as standing mementos.

At the same time the roads will be hollowed and traversed by
chasms, natural arches, and subterranean holes, of the strangest
form, too frequently proving dangerous to the rider passing over
them. ‘These effects, in general only seen in miniature elsewhere,
present themselves on such an immense scale as to leave a very
decided impression on the observer.

4. Volcanic Rocks.—Although these rocks are occasionally more
recent than any of the deposits previously treated of, and are in places,
as from the voleano of Ariquipa, &c., ejected at the present day,
still it is preferred to consider them in this sequence, from the epoch
so assigned to them being one in which they appear to have attained
their maximum development, and in which they have produced such
grand changes in the configuration and level of this part of South
America.

They are, as seen in Section No. 2, contemporaneous with the great
diluvial formations at La Paz, and possibly may there represent an
early Tertiary period, from which time to the present they seem to
have been in more or less continuous activity, and to have presented
themselves with the same general characters and under very similar
circumstances.

M. d’Orbigny* has classified these rocks as of two distinct ages,
known by their differing slightly one from another in their state
of aggregation and the presence of augite. An attentive study of
these volcanic deposits showed how difficult it was to draw any such
detined line of demarcation in rocks which, as before stated, possess
all main features In common; and in fact seemed to show that M.
dOrbigny’s two classes are in reality (at least in many cases) one
and the same, presenting slight differences in mineral character on

* M. Pissis also, Annales des Mines, 1856: “Recherches sur le Systéme de
Soulévement de ? Amérique du Sud.”

1860.] FORBES—BOLIVIA AND PERU. 23

account of the one being subaérial, or injected between the strata,
whereas the other has been subaqueous, and in consequence is fre-
quently met with as a tufaccous bed interstratified with other strata
of acknowledged sedimentary origin. As both such rocks might be
at one and the same time in course of formation, this difference can
hardly be looked upon as indicating a difference in geological age.

The Sections Nos. 1 and 2 (PI. a) are fully sufficient to show
how important a part volcanic action has taken in altering the con-
tours of the mountain-ranges here traversed: probably in no part of
the world do we find voleanic phenomena more energetically developed
or affecting so great a territorial area.

As will be seen from the accompanying Map (PI. I.), the volcanic
rocks forming at the north the active volcano of Ariquipa and others
in that neighbourhood are cut through in Section No. 1 (PI. I1.);
and still further south, in Section No. 2, they form the volcano of
Tacera or Chipicani, 19,740 feet above the level of the sea; still fur-
ther south they form the more or less active volcanos of Sajama
(22,915 feet), Coquina, Tutapaca, Tucalaya, Isluga, Calama, Ata-
eama, Licancau, Toconado, Llullayacu, andl Biers intermediate,
high, in conjunction, form an almost continuous range of volcanos
into that part of the Desert of Atacama pertaining to Chile, through
which country we find this volcanic range appearing at intervals ;
and still more to the southward it is doubtless in connexion with
the volcanos of Patagonia, the north of Magellan’s Straits, and Terra
del Fuego. As will be seen from this, the general direction will
be nearly north and south; and, from a study “of the line of fracture
and position of the intruded rocks, it would appear that the sub-
terranean force here exerted had its centre to the west of this line,
and had acted at a high angle from the west towards the east.

The beds of trachyte and trachytic tuff which are seen interstratified
in the raised beach at Tacna, Azapa, &c., and also in the great diluvial
formation of La Paz, have already been noticed. Further east, in
Section No. 1, at Tarocache, a very peculiar volcanic conglomerate and
tuff stratum was met with, remarkable for the columnar structure
which presents itself on a very large scale on the side of the nearly
perpendicular hill under which the road passes; the columns are so
well developed, that, seen from the road, they look as regular as
similar basaltic formations. On Section No. 2, at Palca, and still
further east, at Questa Blanca, deposits on no great scale, of a white
crumbly trachytic tuff, composed of more or less decomposed felspar,
with quartz and hexagonal black or brown mica-plates and an occa-
sional speck of augite, are met with as more or less horizontal beds,
resting unconformably on the highly inclined strata of Liassic shales,
&c.; both of these deposits, as well as the previously mentioned one at
Tarocache, appear to be remnants of some more extensive bed of sedi-
mentary origin formed of volcanic tuff and ashes from the volcanos
situated still higher up the range.

In Sections N os. | and 2, the great volcanic formation is seen a
little further to the east, forming” a high ridge or range of peaks
aycraging from 16,000 to 19,000 fect above the sea, visible from the

24 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

coast, and generally having their summits coated with snow. In
both Sections (Nos. 1 and 2) this range breaks through the Upper
Oolitic series of shales, claystones, porphyry-conglomerates, tuff, and
mbedded porphyries, and above Tarata has enclosed, or at all events
dislocated, a large mass of these (seen in Section No. 1), in which
several strings of copper-ores were noticed: the volcanic rocks here
are continuous with those forming the volcano of Chipicani, seen on
Section No.2. This I have not ascended; I have only passed along
the sloping plain at its base, the fragments of voleanic rocks on
which left no doubt of its character. Before coming to Uchusuma I
noticed a step-like series of trachytic tufaceous beds, so characteristic
of this rock when met with in this part of the world, each step being
apparently a bed of great extent, and varying in thickness from 10
to 30 feet: these are called ‘‘ Ancomarea” by the Indians, from
their white colour; they extend nearly to the River Caio, at which
place their formation is well illustrated im Section No. 2. It would
appear that they had been erupted through long narrow fissures or
dykes and poured out over the country either as lava or, in some
cases, as light volcanic ashes* emitted from the fissures, and de-
posited on the ground in their neighbourhood, where they have gra-
dually consolidated into beds. At the Rio Cano two such fissures
are seen, bearing nearly i. and W., and dipping 15° to the south, the
more western of which can be traced for miles as far as the eye can
reach, appearing as a narrow white band or ridge, elevated one or
more feet above the ground, from its having resisted the atmosphere
better than the porphyry-conglomerate through which it breaks.
Sometimes, as at the Rio Mauri (Section No. 2) and Chulluncayani,
these are seen capping the rocks, and presenting the appearance of
white bands running along the precipitous flanks of the hills or
ravines; at Pisacoma, Section No. 2, this is also seen, as well as
the occurrence of similar bands injected between the beds of the
red sandstones, and sometimes continuous for miles. As might be
expected, the contrast in colour between these white trachytic rocks
and the dark-coloured Oolitic or Red Sandstone rocks which they cap,
or with which they are interstratitied, frequently at an immense height
up the nearly perpendicular sides of these rugged and barren moun-
tains, is wonderfully characteristic, and visible at very great distances.
When breaking through sedimentary rocks, these lateral eruptions
appear in gencral to conform themselves to the line of stratification,
evidently from this affording less resistance, and there being always
amuch greater tendency for a fissure or crack to follow this line than
to break through the more solid beds.

Between the Oolitic series and the Permian or Triassic sandstones
in Section No. 1, as well as between these last and the Carboniferous
basin of the Lake of Titicaca, we find great tracts which to the passer-
by present to the eye no signs of other rocks than volcanic, and are
occupied by plains or low rounded hills, covered on the surface with
abundant fragments of trachyte and trachydolerites or with volcanic
alluvium, composed of grains or sand of colourless quartz, white or co-

* Frequently containing much pumice.

1860. | YORBES—BOLIVIA AND PERU. 25

lourless felspar, hexagonal brown or black mica, and black or green-
black erystals of augite, along with black magnetic oxide of iron, always
found as a black magnetic sand when a magnet is drawn along the
surface. In passing over these plains the traveller’s attention is at-
tracted, and his eyes dazzled and wearied, by the glittering specks
arising from the reflection of the sun’s rays from the numerous small
quartz-crystals strewed along the surface. The solid volcanic rock
is only occasionally met with ; but hillocks are frequently seen which,
judging from their surface at least, are entirely composed of larger
masscs or fragments of trachytic and trachydoleritic rocks. I do not
consider these tracts as representing spaces occupied by the actual
protrusion of volcanic matter, but in some cases regard them as only
covered by sheets of such trachyte or trachydoleritic lava poured
out from longitudinal dykes or fissures such as before described ; and
in other instances I even suppose them to be, in part at least, composed
of volcanic ashes, tuff, or débris, spread over the surface by the action
of water*.

As far as I could observe, the volcanic rocks do not anywhere
appear breaking through the Silurian rocks; but in the north of
Bolivia they are seen on the Map (PI. I.) as cutting through the
Devonian series near Hachecache and the Lake of Titicaca, a di-
stance of more than 200 miles from the coast in a direct line: this I
believe may be considered as the most inland point at which volcanic
phenomena make their appearance on the western side of the high
Andes. These rocks are all in situ, and are true trachydoleritic and
felspathic lavas which have broken through the strata, part of which
are 1m consequence greatly altered. These lavas are further charac-
terized by the peculiar parallel arrangement of their mineral con-
stituents, which give that ribboned appearance due to the strive of
fusion, such as are frequently seen in more recent lavas.

Professor Philippi having allowed me to examine a series of rock-
specimens which he had procured during his travels in the desert of
Atacama, I found that the volcanic rocks from Punta Negra, Tilopozo,
Toconado, Sorras, Atacama-Alta, &c. were all trachytes or trachytic
tuffs, and precisely identical in mineral composition and character
with those from the more northern part of Bolivia which I have
more specially examined; and from his notes, which he also kindly
placed at my disposal, I find that from San Bartolo to Chanaral
Bajo, a distance of about 250 miles, we have, as in Sections Nos. 1
and 2,a ridge formed by an almost continuous series of lateral
outbreaks of such lava cutting through and flowing over the dioritic
rocks and the porphyries, shales, dc. of the Oolitic series, which, as at
Chaco and other places, contained in abundance Liassic Posidonie,
Ammonites, &e.

The large lateral overflow of lava, from 25 to 30 miles long and
several miles in breadth, extending from San Bartolo to San Pedro

* The plain at Santiago de Machaca, Section No. 2, contains much voleanic
alluvium, as described, and seems rather to have been formed by such aqueous
action. I did not find sufficient evidence for colouring it as a sheet of trachytic
Java, as M. Pissis has done.

26 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

de Atacama, is composed of a trachyte or trachytic tuff, consisting of
a white or flesh-coloured felspathic base, in which are imbedded
plates of hexagonal brown or black mica, and numberless perfect
crystals of colourless quartz from +th to #ths of an inch in length
and having both ends terminated by perfect pyramids ; these quartz-
crystals can be extracted from their matrix, leaving a perfect mould
in the felspathic base, from which they had evidently been the first
mineral element to crystallize.

The trachytic lavas of the other parts of Bolivia and Peru very
commonly show the quartz so crystallized ; and in Sections Nos. 1 and
2 such are also met with, but not so beautifully developed as from San
Bartolo southwards. Both at Atacama-Alta, Toconado, Sorras,
Tilopozo, and other places along the line of Dr. Philipp’s route, the
specimens also showed characteristic trachytic tuffs and trachy-
dolerites. In some of the tufts the quartz present was in the form
of rounded grains, as if due to attrition, or more resembling the effect
which igneous action would produce in rounding off the edges by
fusion, or by the solvent action of some fluid compound i in the lava
acting on the crystals once formed.

There is but little variety met with in the volcanic rocks of this
part of the world, those of Peru, Bolivia, and Chile being all very
similar in external appearance and mineral composition: the principal
rocks are trachytes, trachytic tuffs, trachydolerites, dolerites, and
felspathic lavas.

The trachytes and trachytic tuffs are generally white, but occasion-
ally of a pale flesh- or fawn-colour, and are composed of a felspathic
base, probably only consisting of one felspar (frequently crystallized,
but also met with in a more amorphous form), colourless quartz (al-
ways cryst eae often,as described, in perfect crystals), and black
or tombak-brown mica crystallized in small hexagonal plates, seldom
more than ;4th of an inch across. From the smaller lateral fissures
the eruptions are generally composed of trachytes; but it is extremely
difficult to draw a line between the true trachyte and the trachytic
tufis formed from them, and which occasionally are met with as
solid and compact as the original trachytes themselves, and only to
be distinguished from the latter by the somewhat decomposed ap-
pearance of the felspar, the bronze-brown colour of the originally
black mica and the included fragments of pumice, &c.*; they are,
however, in general much more open or porous in texture, and often
crumbly, so as frequently to be mistaken for white sandstones. They
are everywhere largely quarried and used as building-stone, being
durable and very easily worked; when cut into hollow cones they
are used as filtering-stones for purifying water for domestic use, for
which purpose they are well adapted from their porous texture. I
have reason to suppose that these trachytes have frequently been

* T had expected that the decomposition of the felspar would probably give
rise to the formation of alkaline or earthy carbonates in these trachytic tuffs, and
so afford a means of distinguishing them from trachytes ; in as) I was disap-
pointed, as several trachytic tuffs from Tacna, Azapa, ae Paz, &e., on being
treated with acids did not effervesce at all.

1860. | FORBES——BOLIVIA AND PERU. 27

ejected whilst in a pasty state, after the quartz had erystallized
and the temperature of the whole had become much lower than the
fusing-point of the entire rock itself.

The trachydolerites differ from the trachytes only in having, in
addition to the felspar, quartz, and mica of the latter, crystals of dark-
green or black augite scattered through the mass, in which also the
quartz does not appear so predominant ; and the rock is frequently
considerably darker im colour. They form eruptive masses much
greater than the pure trachytes, and are seen largely developed on
Section No. 1 at Batalla and Yunguyo.

Doleritic rocks I have only met with i situ on the eastern
declivity of the volcanic range of mountains between Tarata and the
River Mauri in Section No. 1; and in Section No. 2 they are seen as
abundant large blocks scattered over the slope of the volcano of
Chipicani. From their very compact structure, conchoidal fracture,
and dark bluish-grey or greenish-grey colour, they much resemble
basaltic rocks; but their crystallization is so close-grained that I
could not distinguish whether olivine was present ; and, in fact, their
mineral composition is not recognizable by the naked eye, so that
their exact nature is open to inquiry: they do not appear to form
any great proportion of the mass of volcanic rocks here developed.

The greater volcanic rocks, at least those which have broken
through as lava and remain 7 situ as a compact rock, are composed
of a crystalline felspathic lava, much more basic in chemical character
than the others (possibly if we except the dolerites), and which ap-
pear to be almost exclusively composed of one or more varieties of
felspar. They generally possess that peculiar parallel structure fre-
quently met with in allvolcanic rocks, whether recent or more ancient,
and apparently due to a cause similar to that of the striee of fasion
visible in glass. This striated appearance is frequently rendered
more apparent from the different layers being of different shades of
colour, reddish or whitish grey, or, as at Pailumani, where these
rocks are very largely developed, of a dark grey colour, probably
from some admixture of augite in a non-crystalline condition and
ntimately diffused through the felspathic mass so as not to be
visible to the naked eye. ‘These rocks sometimes are also found to
contain a little mica or augite, in plates or crystals, but appear in
general to be free from quartz. They are developed on a large
scale between Hachecache and Tiquina, Section No. 1, and also at
Pailumani, Section No. 2, where they appear to form the entire mass
of the eruptive rock,

In neither Section No. 1 nor No. 2 do we cut across any volcano at
present in activity, nor meet with any lava or scoria likely to have
been produced more recently; at but very short distances, however,
both to the north and south of these lines of section, voleanos were
observed in activity ; and during my residence in the country, the
** Misti” or Volcano of Ariquipa vas in eruption. In the immediate
vicinity of Tacora various Solfataras might be seen in action; and
their action on the Oolitic and Porphyry series was visible at ‘ereat
distances, on account of the brilliant yellow, red, and brown colora-

28 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

tions produced by the action of the voleanic fumes and acid vapours
on these rocks, and the formation of various salts of iron, lime, &e.
To the south of Tacora I noticed an evolution of smoke, as if from a
similar solfatara; and my fellow-traveller, M. Friesach, informed
me that, when he passed in October 1859, a volcano situated a little
to the right of Sajama, and apparently one of the three cones named
Las Tetillas on the new map of Bolivia by Mujica and Ondarza, was
observed by him in eruption, vomiting forth immense volumes of
smoke, and apparently also lava, not from the cone itself, but from a
lateral orifice situated at the base of the cone. The volcano of
Tutapaca is also situated in this direction, and is still in activity;
and near this place M. Modesto Bazadre informs me he visited a
valley containing several hundred of little voleanic cones emitting
boiling water, and in many respects resembling the Geysers of
Iceland ; like these latter, the cones around the orifice of ejection are
formed by the deposit from the water itself.

Although we find the volcanos of this part of South America pre-
senting themselves as lofty cones, rismg high above the surrounding
plateau, we do not observe in general that crater-form of summit so
usual in mountains of this class in other parts of the world: we
certainly find, as in the Misti (or Volcano of Ariquipa), some well-
developed small craters ; but these seem rather to have served as so
many safety-valves to the volcanic boiler, and to have played but a
very subordinate part in furnishing the great amount of lava and
other voleanic matter here met with, which appears in greater part,
if not entirely, to have made its way up through the great lateral
fissures or openings (similar in many cases to dykes) which appear
to have poured forth sheets of lava, covering vast areas of the sur-
rounding country. This class of eruptions appears peculiarly cha-
racteristic of the Pacific side of South America, where they seem to
attain a magnitude unknown in any other part of the world. The
southern part of Bolivia shows such lateral eruptions, covering the
ground with trachytic lava for more than 300 miles continuously ; and
in the northern part, as seen in Sections Nos. 1 and 2, the same occurs,
—some of these eruptions appearing to proceed from such lateral
dykes or fissures, at the lowest estimate not less than fifty miles in
length, if not much more.

The. volcanic rocks here described are strikingly distinct from those
which I met with during my examination of the volcanic islands of
the Pacific Ocean and Poly nesia: these latter are generally of very
dark colours, are of a very basic chemical nature, and characterized
by the abundance of augite and olivine and the absence of quartz ;
whereas here in Peru and Bolivia the rocks are invariably of lighter
colour, generally even white, are of a ‘much more acid or siliceous
chemical nature, contain abundance of quartz, and only in some
instances was olivine at all met with.

Before concluding this notice of the volcanic rocks, I may direct
attention to a point connected with the crystallization of the same,
and which, I believe, has not been previously noticed: I allude to the
occurrence in the trachytic and trachydoleritic rocks of perfect

a

1860. | FORBES—BOLIVIA AND PERU. 29

erystals of quartz distributed in abundance throughout the solid and
compact rock-mass. In many instances, as, for example (as before
mentioned), in the northern part of the Desert of Atacama, the greater
part, if not the whole, of the quartz contained in the trachytic beds is
so crystallized, and may easily be detached from the matrix as small
six-sided prisms, terminated at both ends by pyramids, and beautifully
smooth and lustrous. This could not have occurred unless the
crystals had been formed whilst the rock was in a perfectly liquid
state, and before the other mineral constituents had commenced
solidifying.

This seems to point out one great distinction between volcanic and
plutonic rocks. In the former case the quartz has been the first
mineral element to crystallize from the liquid lava, as might
naturally be expected from the much higher temperature requisite

‘for its fusion. In the plutonic rocks (granite), however, the reverse
is the case ; the quartz has been the last element to assume the solid
state and crystallize, and is not found in true crystals, except where
the occurrence of drusic cavities or cracks in the solidifying rock
have accidentally occurred—and even then we only find the one end
of the crystal terminated by planes,—whiulst at the same time the
easily fusible felspar has invariably crystallized before it. It is
evident that in these rocks the quartz has remained fluid or viscid at
a temperature much below its point of fusion, as it occupies the
spaces or intervals of the network formed by the crystallization of
the other constituent minerals of the rock, which are infinitely more
fusible than the quartz itself.

5. Dioritic Rocks.—In geological age, the next rocks which we
come to are the diorites, seen in Sections Nos. 1 & 2, and which may
be termed Post-oolitic, from their cutting through the strata here
representing the Upper Oolitic series.

They are composed exclusively of a white felspar, together with a
more or less dark-green hornblende; the rock itself is generally
coarsely crystallized, but occasionally becomes so fine-grained in
texture as to admit of its being termed a greenstone.

This rock is the same as that which occurs in Chile, and which has
been described by Darwin in his ‘ Report on the Geology of South
America,’ under the name of «« Andesite.”’ I have preferred the name
‘“«TDiorite” until chemical examination may prove it to be distinct ;
as in external appearances it cannot be distinguished from the ordi-
nary diorites of Europe and other parts of the world.

Quartz is never found in this rock when normal; but at one or
two places, as, for example, Cerro de las Esmeraldas and Comanche,
where this rock breaks through the red sandstone beds, the d‘orite
near to the point of contact occasionally contains some little quartz
grains, which it evidently has absorbed from the rock through which
it has broken; in such cases a specimen might be obtained which is
mineralogically, but not geologically, a syenite.

The felspathic constituent is generally of a pure white colour,
and triclinic in crystallization; but, as anorthite, albite, andesine,
labradorite, and oligoclase also pertain to the triclinic felspars, it

30 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,7

will require a chemical examination to determine its nature satis-
factorily.

These dioritic rocks show themselves as a series of more or less:

detached or isolated patches of rock, protruding themselves through
strata of various ages older than the Cretaceous period, which last-
mentioned system appears to be of still later geological age.

On the Pacific, or western side of the high Andes, from Peru to
Puerto Montt in Southern Chile, a distance of some forty degrees of

latitude, we find at intervals such diorites breaking through the

other rocks; and lines drawn through the poimts at which they
make their appearance show that there are two parallel systems of

eruption running not far from north and south, and probably at a

distance of about 100 miles from one another.
In the part of South America forming the subject of the present

memoir, the most western of these lines commences from a little to -

the east of Paposo, in the Desert of Atacama, passes through the
metalliferous district of El Cobre, runs along the cliffs at Cobija, and
touches the coast at Gatica a few leagues to the north of Cobia;
then passing through Tocopilla, Algodon Bay, and the Ansuelo Rocks
near Iquique, again enters the mainland, and, after showing itself at
several points before coming to Arica, is seen in Section No. 2 at
Chuntacollo and Guanuni, and still further north in Section No. 1,
between Tarocache and Tarata; and, from what I can learn, it shows
itself still further north in Peru, and appears to run right through
South America.

The eastern line of eruption, after breaking through the Lias-
rocks between La Encantada and Sandon in the Desert of Atacama,
shows itself at several pots before coming to Tilopozo, from which
place I have specimens brought me by Dr. Philippi; entering the
central part of Bolivia, unexplored as yet by any geologist, it shows
itself at the Cerro de las Esmeraldas south of Corocoro, and the
Hill of Comanche to the north of that place; and, from a specimen
sent me, it must appear in the neighbourhood of Tio Guanaco, at
the southern extremity of the Lake of Titicaca, beyond which I have
at present no data for following it further north.

The eruption of these diorites appears to have been generally
accompanied by the evolution of much acid vapours, probably sul-
phurous, to judge from the effects produced on the rocks in imme-
diate contact with the diorites; as, wherever they break through
sedimentary strata, these latter are much changed in appearance
and chemical composition.

Thus we find the Lias-shales and porphyritic clay and mudstones

converted into a pure white matter resembling china-clay, by the*

abstraction of the lime previously contained in them; and when
this change has proceeded a step further, and, besides, the lime has
also removed much of the alumina present, we find these rocks con-
verted into siliceous or hornstone-like compounds, which have by
several observers been regarded as rocks entirely distinct from those
from which they have originally been deriv ed: thus the quartz-
porphyries of M. Domeyko and M., Pissis are of this latter character ;

ad

1860. | FORBES-—BOLIVIA AND PERU. ayib

and the Tofos mapped on ut Domeyko’s geological map of Chile in
the ‘Annales des Mines’* pertain to the former. Both of these
classes can be seen at many points in the district here treated of, and
will be subsequently noticed.

This rock is occasionally itself metalliferous, as at El Cobre in the
Desert of Atacama, where the diorite is very strongly impregnated
with sulphurets of iron and copper. We always find, however, that
the fissures or faults formed in the neighbouring strata by the pro-
trusion of the diorite are converted into metallic veins by the injec-
tion of metallic compounds of sulphur and arsenic ; and a very careful
examination has shown that the metallic veins of the Oolitic and
Porphyry series of Chile, Peru, and Bolivia, which constitute the
great source of mineral wealth of these countries, are all due to the
appearance of this rock. The silver-mines of Huantajaya and the
copper-mines of Paposo, El Cobre, Cobija, Gatica, Tocopilla, La
Portada, and the veins of iron- and auriferous pyrites frequently met
with, are all of this origin.

In these mineral veins I have found the following metallic com-
pounds to occur :—

Native Gold. Silver-glance.

» Silver. Galena.

» Antimony. Zinc-blende.

» Bismuth. Copper-glance.

>, Arsenic. Copper-pyrites.

», Copper. Erubescite.
Arquerite. Cuproplumbite.
Amalgam. Stromeyerite.
Bismuthic Silver. Iron-pyrites.
Magnetite. Marcasite.
Specular Oxide of Iron. Covelline.
Domeykite. Molybdenite.
Darwinite. Mispickel.
Algodonite. Danaite.
Discrasite. Glaucodot.
Copper-nickel. Pyrargyrite.
Cobaltine. Proustite.
Realgar. Enargite.
Stibnite. Tennantite.

Sulphuret of Bismuth.

And further, from the oxidation of the above minerals, the action of
the carbonic acid in the atmosphere, and the elements in the salts
contained in the sea (under which this country has been submerged
since the appearance of these veins), we also find the following
minerals subsequently produced :—

m Malachite. Condurrite.
Azure Copper. Silicate of Copper.
Atacamite. » of Copper and Manganese.
Sulphate of Copper. Oxide of Copper.
i of Iron. Chloride of Silver.
Tron-alum. Chlorobromide of Silver.
Manganese-alum. Bromide of Silver.

Botryogen. Iodide of Silver.

* Quatriéme série, vol. ix. 1846.

32 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

A little to the north of Cobija, where, from the configuration of
the coast, the line of dioritic eruptions previously described runs
into the sea, we find these forming small pointed or rugged rocks
jutting up from the sea, as has been noticed and figured by Von
Bibra* and D’Orbigny ft.

M. d’Orbigny even supposes these form part of the rock “la plus
ancienne de l’ensemble,” and as pre-existent to the upheaval of the
Cordilleras. A careful examination, however, proved to me that they
are only, as before stated, a part of the general line of diorites, and
consequently younger than the Oolitic series which at these very
places they penetrate into and alter as before described.

The diorites on Section No. 2, at Chuntacollo and Guanuni, are
classed and coloured by M. d’Orbigny as granite, thus confounding
under one head rocks which, beyond their common igneous origin,
are neither in external appearance, mineral character, chemical com-
position, nor geological age in any way allied. As far as my re-
searches have gone, I have not met with any granite in South
America which can be proved to be of later geological age than the
Devonian period.

6. Upper Oolitic Series with interstratificd Porphyritie Rocks.—
The sedimentary beds which here represent the Upper Oolitic system
are so interstratified with beds of eruptive porphyries, porphyritic
tuffs, and porphyry-conglomerates evidently contemporaneous, that it
is quite impossible to draw any lne of demarcation between these
rocks; and therefore I have followed the arrangement of Darwin in
Chile, in placing all the analogous rocks of Peru and Bolivia under
one head. Besides the above-mentioned porphyry-tufts, conglome-
rates, and interstratified porphyries, we meet with claystones, mud-
stones, argillaceous shales and limestones, and other beds, many of
which bear a striking resemblance to the rocks of similar age in
Europe. In the south of the district here treated of, we find these
rocks abundantly fossiliferous ; and the fossil shells from the beds of
the Desert of Atacama have yielded to the researches of MM. Bayle
and Coquand+, and Dr. Philippi, about thirty-three species of recog-
nized Oolitic forms. My collection from the same regions contains
a number not yet examined, and probably will yield further species.
In the part further north the country has been almost entirely unex-
plored, and the fossils obtained by me as yet have only been Litho-
trochus Andii, Ammonites Domeykii, A. pustilifer y Oolitic a
a Gryphea, and the cast of a Trigonia, as well as some vegetable re
mainss.

These beds are continuous from Chile right through the Desert of
Atacama; and, in combination with the focal ev idence there can be*

* “ Die Algodon mee in Bolivien,’ Denkschriften der k Akad. der Wissen-
schaft. Wien. “Math.-2 Nat. Cl. vol. iv. 1852.

+ Voyage dans Y Amérique Meéridionale: Géologie, p. 97.

+ Mém. Soe. Géol. France, deux. sér. vol. iv. part. LETTS he

R I have not here considered it neces sary to go into details as to the fossils,
heik as my own collection from the Desert of INigesan has not yet arrived,
and because most of these more properly belong to Chile, and will be considered
in my next communication when treating of that country.

1860. | FORBES—BOLIVIA AND PERU. a)

no doubt as to the extensive development of this formation, which,
throughout its whole extent, is strikingly uniform in all other
characters.

The thickness of these beds is very considerable; but it would be
too hazardous to venture any estimate of its magnitude without
more decided data than are at present at my disposal. The area
occupied by these rocks, as seen in the accompanying Map, is likewise
very great; and we find that nearly the whole of the coast-line is
formed exclusively of the above-mentioned rocks, which here form
the ‘Cordilleras de la Costa,” whilst in Chile they constitute the
back range, or “‘ Cordillera de los Andes,” a nomenclature which has
caused some confusion, and has been the main cause of the inaccuracy
with which the mountain-chains of this part of South America has
been delineated by geographers.

If we except the small strip of land at Mexillones and the in-
cluded dioritic eruptions, we find that the whole coast-line of Bolivia,
and as far north as Arica in Peru, is formed of these rocks. At
Cobija, in Section No. 3, the Upper Oolitic beds and porphyries
strike about N. 20° W. (magnetic), and dip at an angle of 30° east-
ward, from having been tilted up by the dioritic eruption seen‘in
the section, which has rendered metalliferous, and also considerably
altered the nature of, the rocks themselves near to the point of con-
tact. I noticed a vein here containing grey and yellow copper-
pyrites, with a little atacamite, carbonate of copper, &c., showing
itself on surface, bearing N. 60° E., with a dip of 12°8.E., and cutting
through both the dioritic and porphyritic rocks and shales; the latter
were bleached, and at several points converted into ‘“‘ Tofo,” or a
species of clay sometimes of a pure white colour. These clays, as
previously noticed, have evidently been produced by the action of
acid gases accompanying the dioritic eruptions on the felspathic base
of the porphyry-tutis, &¢., and which, by removing the lime and
iron contained in the same, leave behind a more or less pure silicate
of alumina, in the form of a white clay, or “‘ Tofo,” as such are here
termed ; at the same time the volatilization of compounds of iron has
coloured the surrounding rocks with various shades of yellow, red,
and brown.

High up the sides of the mountains in this section, a copper-mine,
called the Manto de Ossa, is being worked on a considerable scale ;
and in this mine the ore does not occur as a vein or lode, but as a
regular bed, in amongst the other strata. The cupriferous stratum
itself has evidently been originally a bed of porphyry-conglomerate,
or breccia, in which the interstices between the pebbles, or, rather,
fragments composing the bed, have been filled up with metallic sul-
phurets, most probably infiltrated or injected from some neighbouring
vein.

Further north, at Gatica and Tocopilla, numerous veins of copper
are worked in these rocks; and at the former place they appeared to
have a general run of about north-east. The Mina del Toldo, which
I examined, showed for many miles a constant strike of N. 80° E.,
dipping about 85° to the west. The metallic compounds in these

VOL. XVII.—PART I, D

34 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

mines were native copper, atacamite, malachite, silicate of copper,
black and red oxides of copper, purple and yellow pyrites, covelline,
sulphate of copper, &c. These minerals frequently contained native
gold in specks disseminated through them, but were stated to be
unusually poor in silver.

The metallic veins which occur near La Portada, in Section No. 2,
and above Tarata, Section No. 2, present features in every way
similar to the above described.

In Section No. 2 is seen probably the best illustration of the
arrangement and extent of the strata composing this formation.
From this it will be seen that, after passing over a series of very
highly inclined and thin-bedded Liassic shales dipping to the west-
ward, we meet with the dioritic rocks of Chuntacollo and Guanuni
breaking through them and altering them at the point of contact.
Above these the same shales, bearing north and south with a dip of
30° to westward, are again met with, and continue, with oceasional
interstratification of porphyries, claystones, and porphyry-conglo-
merates, through Palea, Los Troncos, El Ingenio, Quebrada de la
Angostura, up to Questa Blanca, where they have a north or south
strike, and dip 50° to westward; here they have some beds of white
trachytic tuff superposed upon them, as previously mentioned; and
near this place we find an anticlinal, causing them now to dip to the
eastward, which dip they retain up to the summit of the nearly
15,000-feet high Pass of Huaylillos. Shortly after passing Questa
Blanca these rocks are very much altered, become flinty and siliceous,
and continue so for a considerable distance, bearmg N.N.W., with a
dip of 50° east: im these rocks several old workings are seen on some
strings of copper. The strike of the beds was at these mines found
to be still N.N.W., with a dip of 20° eastward. The change in
mineral nature here noticed is evidently due, as explained in a former
section of this memoir, to the vicinity of dioritic rocks, and conse-
quent metamorphic action produced by the intrusion, which also has
developed the copper-veins before mentioned, and those near La
Portada. The diorite is, as seen in the section, visible at one spot,
and probably is much more extensive than would appear from the
small eruption crossed in the line of section. From La Portada to
the summit of Huaylilos the rocks are nearly all porphyritic con-
glomerates, frequently much altered and siliceous ; and on the slope
to the Rio de Azufre several beds of true interstratified porphyries
are seen before coming to the great volcanic ridge of Chipicani.

Crossing these volcanic rocks, we next meet the strata pertaining
to this formation at the River Cafio, where they present themselves
as beds of purple porphyry-conglomerate, dipping to the westward,
and broken through by the lateral fissures or dykes of trachyte
seen in the section both here and further eastward, at the Rio Mauri,
at which place they cover unconformably the porphyry-conglome-
rates, as seen on both sides of the steep ravine through which this
river passes. The beds here were thick porphyry-conglomerates of a
purple colour and composed of smaller pebbles of porphyry over-
lying beds of porphyry and porphyry-tuffs, which in turn are suc-

1860. | FORBES—BOLIVIA AND PERU. 35

ceeded by a second series of thick porphyry-conglomerates of the
same character as the former ones. In the beds of porphyry-tuff
IT noticed fissures filled with a crystalline zeolitic mineral, probably
stilbite *.

These porphyry-conglomerate beds continue up to the valley of
Pailumani, where they are cut through by the great volcanic mass of
felspathic lava seen in the section; and no trace was then found of
them before coming to the eastern slope of the Pass of Chulluncayani,
where we again meet with a series of porphyries which appear to
belong to this series, and on the top of which I found several
patches of altered red sandstone near Condorana, which evidently
belonged to the Permian or Triassic series further to the east, and
appear to have been carried up by the eruption of these porphyries.

In Section No. 1 another transverse view of the stratification of
this series is obtained, which, however, is not so extensive as the one
just described, owing to the protrusion of the great mass of volcanic
matter to the eastward. The rocks met with in this section are
precisely similar in mineral character to those met with and de-
scribed in the former Section (No. 2), being composed of argillaceous
shales, porphyry-tuffs, conglomerates, claystones, mudstones, and
interstratified porphyries, cut through by dioritic and volcanic rocks,
and at the western extremity of the section dislocated by a series of
faults, which are easily observed on the nearly perpendicular sides of
the great ravine which forms a passage through this chain from
Quilla to the plains of Sama. They are seen to great advantage, and
were easily sketched and followed out, from the occurrence of several
bands or beds of different colours and consistency, amongst which
several thick beds of coarse porphyry-conglomerate were very cha-
racteristic. This section itself will, it is believed, not require further
description, as the general relations of the strata are not very com-
plicated.

At the Morro de Arica, a hill situated to the immediate south of
the town of Arica, and rising perpendicularly from the sea to a
height of about 500 feet above the water’s level, we also find a series
of porphyries interstratified with sedimentary beds, but the age of
which has not been as yet satisfactorily determined.

These beds are coloured by M. D’Orbigny as Carboniferous, from
his having found fragments of Productus in limestone boulders
enclosed in the porphyry of this hill. I have not considered it ad-
visable at present, before more data are obtained, to separate them
from the other strata with which they appear continuous, and which
have yielded Liassic remains ; but I admit that it requires more careful
examination. A sketch-section of this hill, taken by me on my first
visit to Arica in 1857, shows the following features.

Commencing from below upwards, we find at the base a series of
much-burnt and altered shales, thin-bedded, and of a brown colour,
but too much altered to admit of any recognition. Above this is a

* On examination, its specific gravity was found to be 2:14, the percentage of
water contained in it 17-62, and its hardness 3:25 ; before the blowpipe it intu-
mesces, becomes milk-white, and ultimately fuses into a white enamel.

p2

36 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

mass of some hundred feet of intruded augitic porphyry, very cha-
racteristic, and different from all the other porphyries met with in
these parts, from its contaiming black augitic crystals along with
crystals of white felspar, in a brown, black, or grey felspathic base.
Above these are seen shales similar to those at the base, of a red
colour, and asif calcined*; these are succeeded by a black porphyry,
on which rest altered shales, in the midst of which a thin bed of
grey limestone is seen, with very indistinct traces of organic remains ;
above this a red porphyry, with white felspar-crystals and black
specks of augite, succeeded by a second series of shales, with an
intercalated bed of limestone similar to the first; above these shales
a second red porphyry, then a third bed of shales, and, lastly, great
beds of red porphyry and some pebbly porphyry-conglomerates,
which contain agates and nodules of calc-spar, the latter frequently
covered by a coating of a green mineral. I do not at present ven-
ture to pronounce any definite opinion on the true position and age
of these beds, but only think that the evidence of their being Carbo-
niferous is not sufficiently strong to be conclusive, especially when
it is considered that we have no strata of that age anywhere deve-
loped along the coast of the Pacific.

Before concluding these remarks on the porphyries, I may also
notice the occurrence of eruptive porphyries and some stratified por-
phyry-tuffs in the midst of the Silurian formation further inland.
These are seen to the north breaking through the ridge which
separates the valley of Ilabaya from that of Sorata, a ridge which is
in itself so sharp and steep as to make it appear very surprising to
find it broken through by erupted porphyry, which has left the top
of the ridge asa peak of somewhat hardened clay-slate: the porphyry
is of a red colour, with white crystals of felspar.

Similar eruptions of porphyry occur near Oruro, breaking through
the Silurian rocks. The latter are eminently stanniferous, from which
circumstance, at the point of contact of the porphyry with the Silurian
slates at one locality, the tin-ore or oxide of tin was found fused (M.
Kroeber informs me) by the heat of the porphyry to a true white-tin
enamel, such as is commonly made artificially.

In the Cerro de Potosi, celebrated for the richness of its silver-
mines, and situated still further to the south, such porphyries are
again found developed; and further south of this probably they run
into the porphyries of the Desert of Atacama, which are, as before
mentioned, contemporaneous with the Upper Oolitic beds (these emi-
nently fossiliferous).

Drawing a line through these three poimts, which are coloured on
the accompanying Map (Pl. I.), we find they are in one and the
same direction, and have a general bearing of nearly north-west and
south-east.

7. Permian or Triassic Formation.—The rocks now about to be
treated of and considered as representing in Bolivia either the Per-
mian or Triassic formation of Europe, are seen cut through in their

* On the top of these is a bed of saline and recent accumulation, often very
calcareous, and about from | to 2 feet in thickness.

1860. | FORBES—BOLIVIA AND PERU. 37

entire thickness in Sections Nos. 1 and 2, in which, although at first
sight they seem of much greater magnitude, they do not in reality
appear anywhere to attain a maximum thickness of more than
6000 feet, and generally are found to be much under this estimate.
This is due to the great number of folds doubling up the beds,
and also, as seen in Section No. 2 (from Santiago to Nasacara), to
aseries of faults which repeatedly brmg up the same beds to the
surface.

D’Orbigny has in his section across the same line of country
coloured the greater part of these beds as of Devonian age: at Coro-
coro he makes a part of them Carboniferous, and at the Disaguadero
(Nasacara) puts in a little strip of Triassic. As he cites no fossil
evidence for these divisions, and in fact admits that he has no fossils
whatever from any part of this section, this cutting up into forma-
tions beds conformable to one another, and strikingly analogous in
mineral composition, seems unexplainable except by imagining that
here, as generally throughout his ‘ Geology of Bolivia,’ he proceeds
with the supposition that no link in the chain of geological forma-
tions should be deficient.

The strata so classed under these different denominations can in
some instances be shown to be part of one and the same series of
beds, and, taken as a whole, possess all main features in common.

I have therefore not considered myself justified in retaining these
subdivisions, until at least more evidence is produced, and for the
present have grouped the whole of these beds as one series, under
the name of Permian or Triassic. The balance of evidence appears
in favour of the Permian epoch, although at the same time I admit
that the absence of satisfactory fossil-evidence still leaves the ques-
- tion an open one for inquiry.

These beds are penetrated, upheaved, and altered by the linear
eruption of dioritic rocks which runs through the whole extent of
Peru, Bolivia, and Chile, and which are contemporaneous with the
Cretaceous period. The section from Pisaca to Comanche shows
an example of this. That they are more ancient than the Upper
Oolitic series, is shown by their having been broken up and ele-
vated by the porphyries which are found imbedded or inter-
stratified in this system, and are inseparably connected with the
same in geological age. At Condorana (Section No. 2) this will be
seen to be the case. Still further north, between Condorana and
Pisacoma, these beds appear to dip beneath the whole Oolitic series ;
but the nature of the ground was not favourable to a perfectly con-
clusive examination.

Fossil plants are everywhere found in this formation; but gene-
rally they are very indistinct. In some places, as at Pontezuelo, large
trunks of trees silicified are found in abundance ; and several speci-
mens of carbonized wood which I procured from the sandstones of
Corocoro are as yet not examined *.

* Since the above was written, sections have been made of two of these woods,
and prove them to be Coniferous; but the structure is too indistinct to allow of
further recognition.

38 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

I was informed that a complete Saurian head had been extracted
from the same beds by M. Ramon Due, but was not successful in
obtaining it, nor some fossil bones and teeth now in the museum of
Avignon, in France, sent there by M. Granier, of La Paz.

These beds are superposed quite unconformably on the Devonian
strata at Coniri (Section No. 2), where the red conglomerates, con-
sidered as the lowest beds of the series, abut against the nearly
vertical Devonian shales.

The mineralogical characters of this system so strikingly remind
one of the descriptions of the Permian rocks of Russia by Murchison,
Keyserling, and De Verneuil, that when reading it subsequently
to my arrival in England, it seemed as if treating of these very
strata.

They consist of red, greenish, and variegated marls, saliferous and
gypseous marls, gypsum beds, along with fine red sandstones, thin
grey pebbly conglomerates,and red conglomerates. The marls are par-
ticularly well developed from Santiago to Nasacara (Section No. 2):
at Laguna del Toro (Section No. 2) and at Corocoro (fig. 2, p. 41),
we have brownish-red sandstones, with indistinct vegetable impres-
sions, capped by thin gypsum beds and variegated marls. The
gypsum beds are frequently of great thickness and extent: in some
places, as at Berenguela, they are quarried to some extent, and pro-
duce abundance of fine alabaster, extensively used for the purposes
of architecture (for example, the fountain in the Alameda of La
Paz, &c.): some of the slabs of this material are so transparent,
that tablets of it, until very lately, have been in general use in
this part of Bolivia as a substitute for window-glass: I noticed that
the windows of the church at Pisacoma were formed of this ma-
terial in slabs of about two inches thick. The sandstones vary from ~
red to brown in colour, and generally are not very compact, much re-
sembling occasionally the sandstones of this formation in England, as
at Pacheta (Section No. 2) we find them lighter in colour, and some-
times yellowish. The conglomerates, when intercalated with the sand-
stones, are generally of very insignificant thickness, often not many
inches across, and contain principally small rounded quartz-pebbles,
of the size of a nut, as at La Guardia (Section No. 1); those at
Coniri are of considerable thickness (probably some hundred feet),
and are of a deep red colour, and consist exclusively of rounded
fragments of quartzites, grauwackes, clay-slates, and granite, all
similar to those found in the eastern division of the diluvial forma-
tion before described, and evidently of the same origin.

As in the European Permians, brine-springs are very common in
this formation ; and the cupriferous sandstones, here so well deve-
loped at Corocoro, Pisaca, San Bartolo, Santa Barbara, &c., appear
as the representatives of the similar cupriferous beds of Russia, the
Thiiringerwald and the Harz ; and a further curious coincidence may
be found in the determination by Mr. Kroeber of the presence of
the rare element vanadium in the Corocoro copper-sandstones,—an
occurrence long known as peculiarly characteristic of the Thurin-
gian Kupfer-Schiefer.

1860. | FORBES—-BOLIVIA AND PERU. 39

As seen in the accompanying Map, this formation extends from
the Lake Titicaca in Peru, southwards, nearly, if not quite, through
the republic of Bolivia, and possibly runs right into the Argentine
provinces to the back or eastern side of the voleanic range of the
Desert of Atacama, and everywhere presents the same characteristic
features. The cupriferous sandstones, for example, which are so
characteristic of this formation, show themselves all along this ex-
tent. Beginning their appearance in the north (in the district of
Puno), they are seen at the Pacheta (Section 2), then at Pisaca, Coro-
coro, Chacarilla, Kl Turco, Santa Barbara, San Bartolo, and even fur-
ther south; and Mr. Villamil informs me that they are also visible
in the district of Andalgalla, in the Argentine republic,—a distance
of fully 500 miles from north to south. The breadth of country over
which they are found is probably from 50 to 80 miles across; and the
Sections Nos. 1 atid 2 show the general character of their transverse
section, exhibiting a series of longitudinal ridges, elevated to no great
height above the general level of the plateau, seldom higher than from
1500 to 2500 feet above it, and formed by a series of anticlinals
es a general strike of from N.10°W. to N.W. with varying

p-
A few of the more important observations of the strike and dip of
the strata met with in Sections Nos. 1 and 2 are here appended :—

Hill east of Santiago de Machaca. Softred sandstones, Strike. Dip.
withsred and white| marls .o.icccsostsctecsoosse nce ses N.10°W. 15° EB.
Hill at San Andres de Machaca. Red and white marls N.20°W. 16° N.E.

Hill east of Nasacara. Red clay, with pebbles and

Compactiredtshalesh Me raaemeccececca th ceccer cea 20° N.E.
Hill further east of Nasacara. Red and purple clays... 10° N.E.
Pacheta de Antarini. Soft red sandstones and red marls N.W. 45° N.E.
Laguna del Toro. Brown-red sandstones, with gyp-

SCOTS LOGI) Gash genennnde ssatenpeberc ioaccsbobepodeccdbac CBee N.W. 50°N.E.
Little east of Laguna del Toro. Red-brown sandstones,

WH, GRY SATE RO IS [DYE sododadodsossoooosoasdbadossonsecess N.W. 70° N.E.
Pacheta. Red-brown sandstones, with cupriferous beds NN.W. 40° W.
Pacheta (further east). Red and yellowish sandstones N.E. 30°8.E.
Pacheta (still further east). Red and yellowish sand-

BLOMES Re eeu a ciuidnacaasie nine be ceiscun dieseclneeaism nas taacouceas 20° S.E.
Ditto. (lO bsAohacudasdessooabbaoode 10° SE.
Ditto. GiLGON SSO rans ted 30° S.E.
Ditto. CT RMo oe saobebndcnddhbeoseaooe N.E. 20° NN.E.

West of Tambillos. Light reddish-brown sandstones,

with finely contorted lamellar structure, and the

stratification marked by rows of peculiar black spots NN.W. 25° N.E.
El Tambillo. Red sandstones ................:000ec0e0ee N.W. 45° N.E.
Between El Tambillo and Coniri. Red conglomerate,

large pebbles of quartzite, grauwacke, and granite,

occasionally a fragment of clay-slate .................. N.W. 40°N.E.
La Guardia (Section No.1). Red sandstone and grey i

pebbly conglomerate, with colourless quartz pebbles = NN.W. 45°S.W.
East of Pisacoma. Thin fine red grey and white sand-

stones and pebbly conglomerates .................-0.06++ N.10°W. 20°S.E.

In the accompanying Map (Pl. 1.) it will be seen that at Penas,
near the south end of the Lake of Titicaca, a small patch is coloured

40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

as Permian, quite detached from the rest of this formation, with
which it has been grouped merely from its general resemblance
in mineral character. It rises in the midst of the eastern plateau
or “ Puna” (as it is generally termed by the natives) as a steep
ridge, broken in the centre so as to form a steep anticlinal, with the
strata dipping respectively to west and eastward. The centre of
this anticlinal is formed of red sandstones with gypseous seams; at
Penas the gypsum frequently occurs in crystalline plates of great
purity ; above these, to the westward, are some beds of coarse red
conglomerate, which, in turn, are succeeded and covered by a second
series of red sandstones. At Pefas the gypseous sandstones which
form the anticlinal have a strike of N. 20° E., and, after dippmg at
a high angle to the east, gradually become less inclined, and rise,
with a reverse or westerly dip, in a little hill to the eastward, thus
forming a shallow intermediate basin; the red conglomerates which
should overlie them do not come to the surface.

The well-known copper-mines of Corocoro (which, besides the
supply for the home-consumption, exported from the port of Arica
in one of the last years washed copper of the local value of
2,450,000 dollars) are situated in the red sandstones of this forma-
tion, and have been worked by the Indians from time immemorial.
They were found in operation at the time of the Spanish conquest,
and since then, up to the present date, have gradually increased in
importance, notwithstanding that many of the mining and metal-
lurgical processes are conducted in a manner more indicative of the
times of the Inca dynasty than of the nineteenth century.

The copper occurs native as metallic grains or larger masses, dis-
seminated irregularly in certain beds of sandstone ; but combinations
of copper with oxygen, arsenic, &c. are also found occurring in a
similar manner to the west of the line of fault ; the metallic copper,
however, is the main object of exploration, and in a state of powder,
resulting from the crushing and washing of the cupriferous sand-
stones, is exported in large quantities to Europe under the name of
“ copper-barilla.” The want of coal or wood in this barren region
prevents the other or mineralized ores of copper being worked or
concentrated to a sufficiently high percentage for exportation,—the
only smelting works in operation for the supply of the country, and
for some little ingot-copper for exportation, being supplied with fuel
from the excrements of the Llamas—it being considered that 100
quintals (each quintal = 101; lbs. English) of Llama dung will
smelt 80 quintals of “‘ copper-barilla*.’ The furnaces employed are

* Owing to a wise provision of nature, the Llamas, when pressed by the calls
of nature, do not, like the sheep, scatter their excrements over the ground at
random, but resort to fixed spots, which they select themselves for the purpose,
which circumstance enables an almost incredible quantity of this material (espe-
cially when we consider that in size the excrements do not materially exceed
those of the sheep) to be collected for the use of the copper-smelters, and for the
general supply of the inhabitants with fuel in a country otherwise destitute of
combustibles. The other animals allied to the Llama (Alpaca, Vicufa, and
Guanaco) also follow this laudable custom.

1860. ] FORBES—BOLIVIA AND PERU. 4]

reyerberatories with two chimneys instead of one as generally used
for coal or wood.

The mode of occurrence of the cupriferous deposits of Corocoro is
shown by the accompanying sketch-section (fig. 2), not drawn to a
scale, but affording a pretty good general idea of the main features of
this important mining-district. In this section the beds of cupri-
ferous sandstone which are known and worked are denoted by
continuous black bands, whilst those supposed to exist, but not yet
proved, are shown by interrupted black bands.

Fig. 2.—Diagram-section of the Corocoro Copper-mines.

123 Fault.

1. Veta del Buen Pastor. 3. Veta Umacoia.

In the centre of the section a great fault is seen bearing nearly
but not quite N.W., and dividing the whole metalliferous district into
two parts ; and on examination
it was found to have produced Fig. 3.—Ground-plan of the Fault.
both a horizontal and a vertical
disturbance in the original po-
sition of the beds. Horizon-
tally, the beds which, if merely
broken and lifted up vertically |
on one or both sides of the fault,
would naturally show parallel
lines of outcrop, do not so; |
but on the right hand or east
side of thefault they are skewed
round, so as to make an angle
of about 10° to the fault and
the outcrop of the beds on the
west side. This will be fully
understood by reference to the
annexed woodcut (fig.3), which
is supposed to represent a ground-plan of the present outcrop of the
lines of stratification on both sides of the fault, and will not require
further explanation.

42 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [ Nov. 21,

Still further westward, at Pontezuelo, out of reach of the imme-
diate action of the fault, the beds were found as follows (commencing
from the westward) :—

N.35° W. Dip.50°8.W. Fine red sandstone beds. Found to
affect the magnetic needle.

N.35°W. ,, 45°S.W. Coarser red sandstones, about 150 ft.
thick.

N.35°W. ,, 45°S.W. Fine laminated and thick beds of red
sandstone.

N.40°W. ,, 45°8.W. Fine grey sandstones.

N.45°W. ,, 40°S.W. Coarse grits and fine conglomerates,
consisting of white quartz-pebbles,
hardened grey, black, and greenish
slates, and fragments of red sand-
stone.

Starting from the westward, over a series of fine-grained red
sandstones, we come upon some coarser and more gritty strata, in
which are imbedded several seams containing copper, visible on the
surface by the green colour acquired by oxidation (they are not
worked, being considered too poor); pebbly conglomerates are then
passed over, some of which are also impregnated with copper; and
we then arrive at the Veta de Buen Pastor, a fine-grained sandstone,
impregnated not only with copper, but also with native silver, dis-
seminated in fine metallic grains through the mass of sandstone.
As the silver is of more value than the copper associated with it,
this bed is worked exclusively as an argentiferous exploration.
The succeeding strata are still coarse grits and fine conglomerates ;
and we come upon the Veta de Rejo, or Veta Copacabana, which
also differs essentially from all the others from being rich in copper
in a mineralized state of combination with arsenic, sulphur, de.
The ore from this mine being very dark in colour, from the presence
of much arseniate of copper, this stratum is frequently termed the
“Veta Negra,” or black vein. Still lower in the same class of beds,
the Veta Remacoia, or main seam of copper, is encountered and
found to produce native copper, disseminated irregularly through a
coarse grit, in grains, irregular lumps, or plates, sometimes of very
considerable size. This seam is considered to have been the most
anciently worked deposit of Corocoro, as it had been extensively
worked by the Indians before the Spanish conquest; at present it
is regarded as nearly exhausted, notwithstanding its extent of several
miles, over which it has been explored. It is probable that by
“exhaustion” is only meant a miner’s mode of expressing that the
depth of the workings and difficulty of keeping them free from water
does not equal the value of the produce.

Below this metallic bed we find some gritty strata, and then have
a characteristic bed of fine-grained crumbly red sandstone of im-
mense thickness, the upper edge of which is seen on the surface
clese to the line of fault. Nothing is now known of the strata,
metallic or otherwise, which may exist in depth on this (western)

1860. | FORBES—BOLIVIA AND PERU. 43

side of the fault; but the metallic beds depicted in the section are
supposed by me to exist, for reasons which will subsequently be
explained.

Crossing now over to the east side of the line of fault, we find an
immense development of the same fine-grained sandstones as those
noticed as composing the last bed met with on the surface to the west-
ward of the fault; and in the lower part of this bed we find developed
a series of metalliferous beds differing considerably in their features
from the ‘‘vetas” (or veins,—more properly, beds) previously de-
scribed as seen and worked on the surface at the other side of the
fault. These, from their being of much less thickness, are called
by the miners “ramos,” or branches; and, for the sake of clearness,
only five of these are drawn in the section, whereas many more exist,
as known by the mining explorations in them: for example, in the
‘«‘ Mina de Cimbani”’ there occur five principal or workable “ ramos ”
and nine lesser ones; and possibly a still greater depth may bring
others to our knowledge.

The strike of these “ramos” is tolerably constant, and only
affected by purely local circumstances ; but the dip was found to be
higher as we approached the fault: thus, in the Mina del Pozo the
following observations were taken :—

Strike N. 25° W. Dip. 80° E.
PeVINGE ZO SMW: itensstli vdeo kre
» N.35°W.. ,, 70°H. (Ramo de San Jose.)
PENG OCI culls Gs, eoo alas
RINGO cu NVispuiiiss: died O.cllire

the angle decreasing with great rapidity as we get away from the
fault, showing that a sort of bend or curve had taken place in the
beds on settling down or coming to rest after the dislocation.

A considerable amount of gypsum is found in the form of strings
or veins, also as small crystalline particles disseminated through
these and the beds of red sandstones of this whole series.

These cupriferous beds are very extensively explored in Corocoro,
and produce a large portion of the supply of copper derived from
this district. The ore obtained from the “ramos” is very different
and in a much finer state of aggregation than that from the “ vetas :”
this probably arises from the latter being situated in the midst of
much coarser and more porous or open beds of grit and conglomerates
of small pebbles. In both cases the ore is seldom continuous for
any great distance, but is found scattered through the metalliferous
sandstones, in irregular patches or spots of a white or greenish-
white colour, full of small grains of metallic copper: the colour of
these spots, forming a striking contrast with the deep red colour of
the rest of the bed, affords, at first sight, a sure indication of the
presence of the metal. This discoloration (for such it evidently is)
seems to indicate some chemical change having taken place, appa-
rently connected with the reduction of the copper to the metallic state,
and the formation of the sulphate of lime (gypsum) in these beds.

An attentive study of this interesting formation has led me to

44 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

the conclusion that this change has been caused by the evolution
of sulphurous fumes, disengaged, and penetrating into the pores of
the strata, at the time of the eruption of the dioritic rocks of Co-
manche and the Cerro de las Esmeraldas, situated respectively to the
north and south of the metalliferous district of Corocoro, and the
protrusion of which through these Permian beds I consider as
having caused the fault itself and the accompanying dislocations of
the strata.

The sandstone I suppose to have been, previously to this disturb-
ance, calcareous, and more especially so in the cupriferous parts, in
which I regard the copper as having been present in the state of
oxide or carbonate associated with carbonate of lime. Sulphurous
acid, by combining with the oxygen of the oxide of copper to form
sulphuric acid, would reduce the copper to the metallic state, whilst
at the same time the sulphuric acid thus formed, acting upon the
carbonate of lime, would produce the sulphate of lime (or gypsum)
invariably accompanying these deposits.

It would have much simplified our ideas as to the geological age
and origin of the occurrence of copper in South America if these
deposits could have been shown to have had their cupriferous con-
tents injected into them at the time of this dioritic eruption, which,
as previously has been stated, is the direct cause of all the copper-
veins which I had previously met with in Peru, Chile, and Bolivia.
The question deserves further investigation; but the-facts in hand
appear contrary to this view, and to point out the copper as originally
present in these sedimentary beds, probably, not as metallic copper,
but in a state of combination, and subsequently reduced to the
metallic state as before explained,—in corroboration of which it may
be mentioned that these dioritic rocks can be everywhere proved to
have been accompanied by a great evolution of sulphurous acid and
other gases, by which the rocks in immediate contact have very
generally been greatly metamorphosed. The supposition that the
sandstones were calcareous is only in accordance with the frequency
of calcareous beds met with in the unaltered parts of this formation.

The eruption of these dioritic rocks may, however, have possibly
been the cause of our finding certain beds (or rather portions of
beds), to the west of the fault, containing metallic silver, and im-
pregnated with arsenic, sulphur, &c., by which arsenides, sulphides,
&e. of these metals have been formed as domeykite, condurrite,
copper-glance, &e.

One of these compounds, occurring in the Veta del Buen Pastor
(previously mentioned), in the form of grey metallic grains dissemi-
nated in the sandstone in a similar manner to the usual occurrence
of native copper before described, was analysed by me and found to
be domeykite, the analysis affording—

@oapperiye) iii... eee 71:13
Siliverdiey.ts 2:6 tit eee 0:46
ATSEMICH Reis) d Ae ce 28-41

100-00

1860. | FORBES—BOLIVIA AND PERU. 45

It would appear very probable that this had been formed in situ
by the action of arsenical vapours on the metallic copper dispersed
in the bed. That such a result can be thus produced may easily be
experimentally demonstrated by holding a small piece of Corocoro
copper-ore over a heated crucible containing arsenic.

Only a certain portion of the beds appear to have been so affected ;
and the spotted portion in fig. 2, p. 41, is supposed to represent
this line of arsenical and other impregnation, from which it will be
seen that the Veta del Buen Pastor and Veta de Rejo are altered
from the surface; but the main bed, or Veta Umacoia, is, I believe,
not affected at the surface; but it is so deeper down, since we find
that the native copper from the Mina Cimbani contains arsenic,
as seen from an analysis which is given a little further on: and I
am informed that silver has been met with in depth in the Mina
de Quimse Cruz; possibly this impregnation of arsenic, silver, &c.
might (or in greater depth be found to) present itself as a vein of
these metals.

The metallic copper of Corocoro is not only found as small grains
in the sandstones, but also in nodules, irregular lumps, and plates
or sheets interposed between the beds of sandstone, occasionally
assuming crystalline and beautiful dendritic forms. In the Socabon
de la Paz, on the Veta Umacoia (main seam), pseudomorphic cry-
stals of native copper are found as hexagonal prisms without ter-
minal planes; an analysis of one of these by Mr. Kroeber is an-
nexed :

Coppermine semen cra: 98:°605
ICA Maer nt nine cannery 0-015
Dilyereentc aces URC eter (trace)
ony (asvlost) neo ee 1-376

Metallic matter (insoluble in
IN OPER C I) Site src aay 0-004
100-000

Some are solid; but others, when sawed through, exposed a nu-
cleus of carbonate of lime, which would lead to the inference that
these pseudomorphs had been formed by the action of a solution of
copper on crystals of carbonate of lime, and by some subsequent
chemical change the carbonate of copper so formed had been reduced
to the metallic state.

As is well known, the Permian Kupfer-Schiefer, or cupriferous
bituminous shales of Thuringia, are characterized by the occurrence
of the rare metal vanadium entering into their chemical composi-
tion; it appeared to me, therefore, of considerable interest to know
whether this also was the case here in Corocoro, where strata oc-
curred of very different mineral character, but supposed to represent
the same geological epoch. Not having a laboratory at my command,
Mr. Kroeber kindly undertook the examination; and his analysis of
the washed copper-ore from the Mina de Cimbani, previously men-
tioned, afforded the following results :—

bs

46 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

Water a) eattioais al Nappi 3°500
Coppers actii iss setae 63°341
TOM Guns Hele eG SUNN 1-200
DUkverr tess ee yee. ary tae 0:003
Sulphunrewacidi yee eee 4-301
Ryu plariy,tcepekeeh gee ee gegen 2-102
IATSEMITG cea Ait A A ae 21-341
Carbonichacid@am eae 4-032
Vanadicwacidaaene eee 0-412
Sandy) hate Vue once yay : 0-100

100-332

from which it will be seen that even here in Bolivia, so far distant,
the same chemical agencies had been in operation, and we find the
metal vanadium playing a geological réle, if such a simile be
allowable.

As the respective names of “ veta” (vein) and “ ramo ” (branch)
denote, the metalliferous beds situated to the east of the fault
had most probably, from their lesser thickness, been regarded as
branches or offshoots of the former,—a supposition apparently sup-
ported by finding in the Mina Cimbani the actual contact of the
former with one of the latter (Ramo de San Prudentio); and a large
hand-specimen in my possession, taken from this point, and kindly
given me by General Brown, the proprietor of this mine, shows, as
in fig. 4, the two inclined at an angle
one to another, strongly cemented to- Fig. 4.—Sketch of the Hand-
gether, and presenting the peculiar specimen, showing the Fault.
characters of each of these different
deposits and the adjacent rocks in
which they are situated. This circum-
stance is naturally due only to the eS
different inclination of the strata on Veta Y
each side of the line of fault, causing
the veta to cross the upper ramos; it
is, however, interesting as showing
how intimately the fault has been closed up by the grinding and
sliding action which accompanied its formation.

Attempts had been, at various times, made by the miners of Coro-
coro to pursue their workings on these ramos through and on to
the other side of the fault, and also to discover the representatives
of the vetas on the eastern side of the same; but researches made
without any preconceived idea of the true state of the case were not
likely to be successful; and, up to the time I left Corocoro, they
had not been attended with other results than pecuniary loss. Time
did not permit of my making a correct section across this interesting
metalliferous district, and so deciding the question ; but a study of the
immediate neighbourhood of the fault, and particularly the discovery
to the west (and close up to the line of fault) of the upper beds of
fine-grained red sandstones, very different from the coarser beds

*

Ramo.

1860. | FORBES—BOLIVIA AND PERU. 47

above them, and so analogous in character to those on the east side of
the fault (and which also I could find developed further west),
furnished me with a clue to the explication of the question as
represented in the section. I have further reason to believe this
to be correct from finding, much further to the west (as marked
in the section), coarser and pebbly beds and traces of the outcrop
of cupriferous beds, which, on examination, may possibly prove
to be the representatives of the western half of the dislocated
paaye teed

Before taking leave of Corocoro, [ must mention the occurrence of
fossil wood in the beds of the mine of Quimse Cruz, in a carbonized
state, and occasionally having the pores filled with metallic copper ;
also the occurrence of a fossil skeleton of a Mammal in the mine of
Santa Rosa‘? in 1859, part of which I was enabled to obtain through
General Brown, and which Prof. Huxley, having kindly examined
it, pronounces to be the skeleton of a mammal of the Camel tribe,
allied to the Llama, but presenting marked differences from it: it
has been called by him Macrauchenia Boliviensist. See p. 73.

The occurrence of a Mammal of the post-pleistocene period in
strata considered as so much older appears only to be accounted for
on the supposition that the animal had fallen into a fissure in these
rocks, and been subsequently covered up by the crumbling sandy
débris of the adjacent rocks, which has gradually consolidated. The
mine of Santa Rosa being situated close to the fault, it might be also
possible that some portion of the fault itself has not been closed up,
and has thus left a fissure, which might account for the depth at
which these remains were found under the surface. The bones
themselves are in some instances almost converted into copper, or
at least the pores are filled with that metal,—a circumstance easily
accounted for in strata so highly impregnated with it.

Thave gone into this detailed description of the cupriferous forma-
tions of Corocoro, because they are at present the object of the most
important metallic explorations in the Permian rocks of Bolivia; but
from all I can learn, the other mining districts in this formation
present quite analogous features, and in some cases, as at San Bartolo
in the south of Bolivia, are developed on an equally large scale,—
the occurrence of the metallic copper in them being exactly as de-
scribed in Corocoro§.

The disturbances or convulsions which have affected the Permian

* T cannot but express here the obligations I am under to Fieldmarshal
Brown, M. Pedro Saienz, and other friends at Corocoro for the kind assistance
they afforded me in my researches in this part of the country.

+ The former of these mines belongs to Mr. Teare, the latter to Mr. Griffiths.

{ The occurrence of an animal allied to the only known larger mammals
of this part of Bolivia (the Llama, Alpaco, Guanaco, and Vicufia) is further in-
teresting as showing that the great Bolivian plateau, at so much earlier a period,
was inhabited by animals generically allied to those found there at present, and
two of which (the Llama and Alpaco) are known to be indigenous, and not to
occur elsewhere in the world.

§ Mr. Abel of Copiapo has, in a letter, kindly forwarded me the following

48 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Nov. 21,

or Triassic strata in this part of the world are referable to three
distinct epochs :—

1. Their upheaval by the porphyries of Oolitic age.

2. The protrusion of the still later dioritic rocks.

3. The eruptions of the volcanic rocks, properly so called.

All these have been already treated of more or less in detail; and
in the sections accompanying this memoir (PI. II.) these occurrences
are in themselves sufficiently obvious to require no further expla-
nation.

8. Carboniferous Formation.—The rocks of Carboniferous age met
with in Bolivia, to the west of the high Andes, appear, at intervals,
as small, elongated, basin-shaped deposits, the longer axis of which
is more or less north-west and south-east; these basins are situated
in the midst of the great western diluvial plateau, showing them-
selves to the north at the Lake of Titicaca, and, further south, in
the provinces of Arque and Oruro.

The portion of this formation examined by me is shown in the
accompanying Map (Pl. I.) and Section No. 1 (Pl. I1.), where it
forms the Isthmus of Copacabana in the Lake of Titicaca, the pro-
jecting headland on the other side of the Straits of Tiquina, and the
islands in the lake itself. Itis of very small extent when compared
to the immense areas occupied by the other sedimentary formations
here treated of; but it is everywhere highly fossiliferous, and pre-
sents a fauna which leaves no doubt as to its geological age: the
lowest elevation of any part of it visible is about 12,500 feet ; and it
ascends from that height up to fully 14,000 or 15,000 feet above the
level of the sea.

The unfortunate circumstance that war was declared between the
republics of Peru and Bolivia when I was in this part of the country
prevented me making anything but a most superficial examination,
As this isthmus is divided between the two nations by such a ser-
pentine line of frontier that in a day’s journey in a straight line the
traveller enters and leaves the territory of one or the other of these
republics no less than seven times, and both lines of frontiers were
occupied by the respective hostile armies, a geologist was placed in
a very suspicious and uncomfortable position—as I had reason to
experience. I was therefore glad to get over the ground as quickly

analyses of the copper-sands from San Bartolo, showing the composition of the
ores found there in the cupriferous sandstone :—

ile 2.
CONOR cep rene. seanmenssenioneese 07:3 343
Insoluble matter are ANG
dione || if ceecesscesse 35-4 50:2
Alumina, Iron, &e. re es
Soluble in acids f "" pth
Carbonate of lime............... 1-4 69
98:5 98-7

the deficiency in the above analyses being due to a portion of the copper being in
a state of oxidation in the ore: thus, in No. 1, 9-9 per cent. of copper were dis-
solyed in dilute hydrochloric acid.

1860. | FORBES—BOLIVIA AND PERU. 49

as possible, and was only enabled to make observations on the imme-
diate route ; so that the section of this basin is to be regarded as a
sketch merely ; but, at the same time, I believe that it represents
pretty accurately the real state of the case.

Starting from the eastern portion of this section, from Hachecache,
after traversing the volcanic rocks and a series of highly contorted
beds supposed by D’Orbigny to be of Devonian age, we arrive at the
Carboniferous series, represented in the section as being unconform-
able to, and abutting up against, the last-mentioned beds, owing to

= e the occurrence of a fault:
this appeared to be the case ;
but I admit that it is not de-
termined with as much pre-
cision as I could have wished.

The strata first met with
are red sandstones covered by
some white sandstones, both
of which alternate with and
are succeeded by a rather
nondescript rock, probably
igneous, as the overlying beds
of shales appeared to be al-
tered as if by such agency ;
above these are some thin
calcareous beds (fossiliferous),
but the fossils I met with were
too indistinct for determi-
nation; and then greenish
shales, compact greenish
shales, and red shales, suc-
ceeded by beds of red sand-
stone, forming the beach at
Tiquina, at the Lake of Ti-
ticaca.

The Straits of Tiquina,
which here separate the lower
from the upper part of the
lake, appear to the eye not
to attain a breadth of more
than from one-half to one
English mile across, and,
from the appearance of the
stratification on both sides,
are most probably the seat
of a great fault which has
broken up the continuity of
the Carboniferous series.

Hitherto in the section
these strata have all shown a dip to the westward, at pretty high
angles, up to Tiquina: on crossing the straits, however, we meet

VOL, XVII.—PART TI. E

1
1
’
'
’
1
1
1
1
\
’

La Guardia.

a
:
'

ated shales, sometimes calcareous.

d blue limestones.

e, e, Thick yellow an
d, d, White and varieg
Red sandstones (with drift-bedding).

b, Red sandy conglomerate.
a, a, White sandstones.

C, ¢,

(Mountain-limestone).

Fig. 5.—Diagram-section of the Carboniferous Basin of Lake Titicaca.
low sandstones.

*—*, Level of the Lake Titicaca.

h, h, Thiek blue limestone
g, Variegated shales.

z, White and yel
f, Sandy shales.

50 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

with red sandstones, apparently identical with those on the other
side, but so dislocated as to present the appearance of the broken
half of an arch; and a few yards further from the beach the beds are
brought to a vertical position; and thus forming a fan-shaped con-
tortion, they commence dipping to the eastward at angles at first
very high, but becoming lower and lower as we proceed westward.
The relations and order of succession of these rocks are, however,
much better seen in fig. 5, showing a section of the Carboniferous
series, from Tiquina to La Guardia, in an east and west direc-
tion. This section appears to represent the entire thickness of this
formation.

The above section will require no further exylanation or descrip-
tion of succession; but with reference to the fossils, I may state
that those which I was enabled to extract from these beds have been
named by Mr. Salter as follows :—

Productus semireticulatus, Martin. Athyris subtilita, Ha//.

(P. Inca, D’ Orb.) Orthis resupinata, Sow.?
Productus Longispina, Sow. (Capacii, _ Andii, D’ Ord.
D' Orb.) Rhynchonella (new species).
Spirifer Condor, D’ Orb. Euomphalus (Phanerotinus ?).
Boliviensis, D’ Orb. | Bellerophon; like B. Uri, Flem.

along with numerous fragments of Corals and Crinoids in too imper-
fect a state to admit of being recognized.

A Phacops, named in Plate IV. Phacops Pentland, was brought
from Aygatchi at the south end of the Lake of Titicaca, by Mr.
Pentland in 1838, and supposed by him to be in the Carboniferous
rocks there ; but, according to Mr. Salter, this is an Upper Devonian
type. It might possibly come from the sandstone series at the base
of the Carboniferous, as the rock in which the specimen is imbedded
seems to point out; in such a case these sandstones may be of Upper
Devonian age.

I have not had an opportunity of visiting the Carboniferous beds
in the provinces of Arque or Oruro; from the former, Colonel Lloyd
some time ago sent home the following species:—*Spirifer Condor,
S. lineatus, Productus Cora, P. Inca, P. Boliviensis, and Orthis Andii.

The Carboniferous rocks of the Department of Santa Cruz appear
to form a perfectly distinct series from the above-described isolated
basins, being situated at a much less elevation above the sea, and cut
off from all connexion with the others by the intervening mountain-
chain of the Andes. According to M. D’Orbigny they are of much
greater extent; and the fossils which I have seen appear in much
more perfect preservation. Mr. Cumming brought to England the
following fossils, stated to be from Santa Cruz :—Terebratula mille-
punctata, Rhynchonella Peruviana, R. Pleurodon, Spirifer Bolwiensis,
and S. Condor.

M. D’Orbigny has coloured on his map as Carboniferous a small
patch around and including the “ Morro de Arica,”’ which is seen in
Section No. 2 as a steep hill rising perpendicularly from the water’s
edge to the height of about 500 feet above the sea. The evidence he
adduces is the occurrence of traces of a Productus in blocks of lime-

1860. | FORBES—BOLIVIA AND PERU. 51

stone brought up by the porphyries which constitute the greater mass
of this hill. This evidence does not appear to me sufficiently con-
clusive to warrant its being separated from the other strata, which
appear continuous, and which are decidedly of Upper Oolitic age,—
more particularly as we have no example of the occurrence of Car-
boniferous beds anywhere along the coast of the Pacific in South
America. I have therefore classed them along with the Upper
Oolitic series until a more careful examination, which I hope soon to
make, may afford data for determining their exact position.

9. Devonian Formation.—The rocks which in Sections Nos. 1 and
2 are represented as of Devonian age have only been so coloured since
my arrival in England: when these sections were made in Bolivia
I had always regarded them as forming part of the Upper Silurian
series, and coloured them accordingly.

I have been induced by Mr. Salter to look upon them as possibly
Devonian, although far from being convinced of their being so in
reality. The evidence of their geological age is as follows. No fossils
were found in the beds of either of these sections by myself.; but
M. D’Orbigny cites one single specimen as occurring near Hachecache,
a new species of Orthis, called by him Orthis pectinata, and re-
garded as decidedly Devonian by him, although Mr. Salter, judging
from the figure and description of M. D’Orbigny, allows that it might
pertain to any formation from Silurian to Carboniferous. The Pha-
cops Pentlandu, from Aygatchi, is from near the junction of these
rocks; but, as previously observed, it may possibly (as Mr. Pentland
supposes) come from the base of the Carboniferous basin, the beds
at the base of which might consequently be of Devonian age; but
the exact locality of this fossil is too uncertain to allow it to be con-
sidered in settling this question. A series of beds of somewhat
similar mineral composition occurs in the same strike as these at
Oruro, in which a white sandstone contains great numbers of an
Orthis considered by Mr. Salter as Devonian or Carboniferous from its
belonging to the group of Orthis resupinata and O. filiaria. The Car-
boniferous series having been also developed, as previously mentioned,
in Oruro, this Orthis might possibly belong to the sandstones at the
base of the same. A Favosites also found near Oruro does not afford
any satisfactory evidence, and we have only one fossil admitted to be
truly Devonian—the Phacops latifrons, found in a rolled pebble in
the diluvial plain near Oruro, and which is believed by Mr. Salter
to agree in all essential particulars with the European and American
species.

Any evidence derived from thickness of strata in a case where the
Devonian, Upper Silurian, and Lower Silurian formations united, as
exhibited in the sections here laid before the Society, are not con-
sidered to attain a collective thickness of more than 20,000 feet, can-
not be taken as in any way conclusive against grouping the whole
of these strata under the Silurian formation, when the magnitude
of similar strata in other parts of the world is taken into con-
sideration.

Having frequently heard of the immense development and thick-

E2

52 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Noy. 21,

ness of quartz-rock in Bolivia before having visited that country, I
afterwards paid considerable attention to this poimt; but in the di-
stricts traversed by me, although containing a vast area composed of
more or less compact sandstones and impure siliceous beds, with in-
terlaminated partings of blue, olive, or brownish-red shales or slates,
I did not meet with any very extraordinary thickness of them.

A superficial observer, particularly if passing rapidly over the
ground, might, in several places, easily be deceived into the belief
that such a thickness really occurred, from finding the strata dip-
ping to one side over a great distance, as, for example, between
Hachecache and Tiquina, where the beds passed over might for this
reason appear to form part of an immensely thick series. As shown
in Section No. 1, these beds are in reality contorted and doubled up
into an almost innumerable series of extremely sharp, small folds ;
and in this case I counted no less than 23 such folds in the short
distance between Hancoamaya and the commencement of the Car-
boniferous series, owing to which the appearance of a very general
dip to the eastward was presented.

In the annexed map (PI. I.) the Devonian series is coloured toge-
ther with the Silurian with one tint, from my being unable to draw
so definite a line of separation as is found in M. D’Orbigny’s map:
their mode of occurrence is so well illustrated in Sections Nos. 1 and
2, that a description would be superfluous.

The strata themselves consist of white sandy beds more or less
compact, yellowish impure sandstones and grits, and, as is seen in
Section No. 1, at Hachecache, quartzite-like rocks, showing them-
selves both to the east and west of that place, and easily recognized
in section from their rugged and shattered appearance, due to their
having been too rigid to bend along with the other beds; interstra-
tified with these are blue, olive-green, or reddish-brown shales, and
beds of blue clay-slates.

Sir Roderick Murchison, some years back, in his ‘ Siluria,’ when
reviewing the Devonian formation of Bolivia as described by M.
D’Orbigny, expressed himself thus :—“ In the absence of sufficient
proof, doubts may be entertained whether these sandstones and
quartz-rocks of the Andes may be of Upper Silurian rather than of
Devonian age ;”’ and my own researches have tended to make me
adopt this opinion: at the same time, however, I think it probable
that there is in Bolivia a true Devonian system at the base of the Car-
boniferous strata, consisting of white, yellow, and brown-red sand-
stones, with intercalated shale-partings, which collectively do not
attain any very great thickness nor occupy any very extensive super-
ficial area*.

* These beds probably are of Upper Devonian age. I have not examined any
part of the country which lies on the eastern slope of the main chain of the
Andes and is coloured by M. D’Orbigny as Devonian. As will be seen from the
comparative sections appended to this memoir (PI. III.), M. Pissis does not en-
tertain the same opinion, but in his section he represents these beds as being
lower in position than the whole of the very thick strata which I am now about
to describe as representing the Silurian epoch.

1860. ] FORBES—BOLIVIA AND PERU. 53

10. Silurian Formation.—The rocks which I have grouped together
as pertaining to the Silurian epoch show themselves continuously, or
very nearly so, over an extent from north-west to south-east of more
than 700 miles ; and the area occupied by them cannot be estimated
at less than 80,000 to 100,000 square miles. They form the moun-
tain-chain of the high Andes, rising to an absolute height of 25,000
feet above the sea, and, in the part of South America more parti-
cularly the subject of this memoir, continuous through Peru from
the north of Cusco over the snowy ranges of Carabaya and Apollo-
bamba, across the provinces of Munecas, Larecaja, La Paz, Yungas,
Sica-Sica, Inquisivi, Ayopaya, Cochabamba, Cliza, Misque, Chayanta,
Yamparez, Porco, Tomini, and Cinti, throwing off spurs along the
eastern side of the main chain, right through the province of Cau-
polican, down to the River Beni in Mojos, into Yuracores, Valle
grande, Santa Cruz and Chuquisaca, and to the east into the pro-
vinces of Oruro, Potosi, and Chichas*. :

Some of the greatest rivers of the world have their sources in this
mountain-chain. The Amazon, with its mighty affluents the Purus,
Madera, Beni, Mamore, Rio Grande, as well as the Pilcomayo and
other branches of the River Plata, are fed by the snows of this great
Silurian region.

In this range also we meet with the loftiest mountains of South
America, second in height only to the Himalayas. Thus we have
Tampu (Sorata) 24,812 feet (25,200, Pentland), Hlmani 24,155
(24,200, Pentland), Huayna Potosi 21,883, Coloolo 22,374, and
many others, rivalling these in height, but the elevation of whose
peaks has never as yet been ascertaincd. These peaks do not, as _
M. D’Orbigny’s published researches would lead us to suppose, con-
sist of mighty cones or bosses of granite, but are in reality composed
of Silurian strata,—fossiliferous, as I have proved in the case of
Illampu (the highest of them all) up to its very summit’.

The Silurian series in these regions present a physical configura-
tion, as well as other features, so unmistakeably analogous to those of
their equivalents in Europe, that, notwithstanding the much grander
scale on which they are developed, the geologist cannot but imagine
himself breathing the air of Siluria, even before an examination of
- the rocks themselves confirms this suspicion.

The extensive development of clay-slate, shales, and grauwackes,
along with the metallic contents of these rocks, present mineral cha-

* T have visited, of course, but a small portion of this vast territory, but have
availed myself of all procurable data and many specimens of the rocks df these
provinces, principally from mining adventurers and others who have explored
these districts, from whom I have received much information and assistance.

+ M. D’Orbigny presents us in section with the lofty Illimani as an immense
cone of granite. When there, I could not find a trace of this rock; and Mr.
Pentland, who ascended the side of Illimani to a much greater elevation than
I did, assures me that he met with only clay-slate, and found no trace of granite
or other eruptive rock. Mr. Horner has also directed my attention to the an-
nexed paragraph in Naumann’s * Lehrbuch der Geognosie,’ 2nd edit. 1858, vol. i.
p.97:—‘‘ Die beiden héchsten Gipfel der dstlichen Andeskette von Bolivia,
namlich der Sorata (19,974 F.) und der Ilimani (19,834 F.), bestehen aus Grau-
wackenschiefer, und sind keine Vulcane.”’

54 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 21,

racters very similar to the Lower Silurian series in Europe, particu-
larly as we do not, as far as I have examined, meet with the lime-
stone beds and calcareous shales generally accompanying the Upper
Silurian series. The examination made by Mr. Salter of the fossils
extracted by me from these beds appears, however, to show that we
probably have the whole Silurian series, from lower to upper, fully
represented, notwithstanding the general uniformity in mineral cha-
racter of the beds.

Starting from the north, at Tipuani, we find this auriferous region
principally composed of blue clay-slates, which, from information
communicated to me, I believe to cover a vast area, extending down
to the River Beni. In these strata no fossils have as yet been found*;
but they appear to be quite continuous with the beds which contain
fossils near Sorata, about five miles south of which town I found, at
a small Indian place called Cotafia, on the east side of the river, an
Orthis (apparently O. Aymara), Strophomena (species undetermined),
Annelid-tubes well defined, and small round bodies of pyrites with
a hole in the centre like the joint of an Encrinite, about one-third
of an inch in diameter, occurring in the blue slater.

Still further south, on the north-west slope of Iampu, I found in
loose stones, at a place called Cochipata, traces of Cruziana Unduavi
(Pl. V. figs. 7, 8), and a little further, at Ucumarini, also on the east
side of the river, Annelid-burrows and the Cruziana Cucurbita (Pl. V.
figs. 4-6). The burrows were of varied forms and sizes, and perfect
counterparts of those from Unduavi in Yungas, although this place
is situated some 120 miles distant on the other side of the Andes.

Still further south I fixed my head-quarters in the Hacienda de
Millepaya, and by extensive excursions from that point, and ascents
as far as possible up the steep western slope of Hlampu (or Sorata,
as it is generally but erroneously termedt, from the town of that
name situated at its base), I was enabled to form the section of the
strata represented in Section No. 1, and to examine the beds as to
their fossil contents. The results of this examination are given below,
premising that above the shales forming the uppermost beds repre-

* Tt requires an attentive search in order to discover fossils in a new country.
The small number of Bolivian fossils at present known is not to be ascribed to the
poverty of the rocks, but to the insignificant proportion which the few isolated
spots hitherto examined bear to the vast area of this republic: as far as I have
explored, this country shows evidence of being eminently fossiliferous. I believe,
however, that I have, during my recent and short travels in this country, brought
home more fossils than any explorer before me, notwithstanding that M. D’Orbigny
and M. Pissis (who lived eight years in Bolivia) had much better opportunity
than myself.

+ I have to thank Mr. Salter for his great kindness in carefully examining the
fossils of the Silurian, Devonian, and Carboniferous series. The names here given
are those affixed by that gentleman, who has communicated a paper illustrative
of the fossils which I brought home from Bolivia. See p. 62.

¢ The mountain itself is called in Bolivia by the original name of Illampu, at
the foot of which, to the north, the town of Sorata is situated; and the snowy
range above this town being frequently called the ‘‘ Nevados de Sorata” has led to
the mountain Ilampu (the highest peak of this range) being called, more parti-
cularly by English writers, Sorata.

1860. } FORBES—BOLIVIA AND PERU. 5d

sented in this section are several beds of a quartzitic sandstone,
which again are followed by the strata coloured as Devonian. The
beds enumerated in the annexed table are numbered from W. to E.,
or in descending order, commencing with the highest :—

Ih.

2.

O00 NIMS Oo

33.

. Shattered blue shales of great thickness
. Thin blue slates at Hacienda de Mille-

. Slightly micaceous blue beds ............

. Siliceous grauwacke sandstone beds,

Thick blue clay-shales .............--.- No fossils found.
Annelid-burrows, some globular

. : ( bodies, and a fossil supposed by
aE ieee ot slates. Strike N.5°W. 4 Mr. Salter to be a Cruciana;
ip OM ene coe RbA Hab ON SaGNeR or oRCHia | also a curious Patella or Pile-

opsis.

. Blue, hard, and slightly micaceous beds Orthis Aymara.
. Less laminated micaceous beds .........
mebluerclay-shalesim. jn neeeetheeeacsece reas
. Blackish-blue shattered clay-shales ...

Thin bed, about 6 inches of slightly

No fossils found.
calcareous shales .......cc0.....00100000-

paya, much jointed ..................0..

Aymara, Cruziana Cucurbita, An-
nelid-burrows, and several indi-
stinct bodies.

Orthis with fine strix. Orthis
\

about 100 feet thick ...................4.

+ «A antray sf] ove 1 Pays ete mapa au eNeiete riod Uy sere

. Grauwacke, thin bed, sandy ............

Me nimyshrallestasstn mee MAN Ney

Me Gran ACK Css ena Hane ee areie yuu nasa No fossils found.
Me Mhimyshalegyesssacsencenesenaconc ence ees |

MAG TAUWACKE 22h «actor aiceselncace ee tanbene

Sines al es ee. ose kcasce cane ees ccaunieeate:
PaGrauwackeyeceaenesnert yas ucacesecgatoe

. Clay-slate, dirty-blue colour ............

. Thin-bedded micaceous clay-slate ...... Annelid-burrows.
OMe WISMS ALESHA Me easel ee eee ce custad eaeeee
doeDhinvgrauwackej.c.esesecscegtecuesneeee
sme Clayeslate atic teisnsi tudes lanewan shew
. Thick grauwacke-slates ................ P

No fossils found.

{ Orthis Aymara, Worm-burrows,

. Rather hard, greyish-blue, sandy shales | Otenodonta (Nucula)

on (OIE ASIEN hecodoobuncasnasbdaseosneadnnnes
mGrauwacke-slates=ssnws.weash tens aeessicel er No fossils found.
. Hardened clay-slates ....................-

. Whitish grey, hard grauwacke-slates, or |

Homalonotus (new species).

GpIaCabye GoeN ES) ooebdebooasasononddcosonpascce
SGramwacke beds ssacotisess stds eee cesee Noa fossil found.
. Micaceous clay-slates ..............000008. Annelid-burrows.

{ Orthis Aymara, Phacops, Proe-
tus, Cucullella, Ctenodonta (Nu-
cula), Arca Brownti, Bellerophon,

Blue siliceous clay-slate, or more or less Tentaculites Satenzit, Raphisto-
sandy shale; weathering white on the { ma?, Homalonotus Linares, An-
BUNTACE YN re ey ara MIN a ee N Les oe kas nelids, and several other fossils,

indistinct. This bed seemed to
abound in the above-mentioned

\ fossils.

. Hard, white, altered clay-slates, ely Be pnenitaltonacan

through by metallic veins...............

56 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

( Tentaculites supremus anda Cup-
| coral; also several indistinct fossils,

35. Similar slates; still more altered ...... { amongst which many bodies about
| 3 to 4 inches long, looking like
\ Orthoceratites.

Lie Sie Homalonotus Linares, Tenta-
36. at pirata jwhttish\ brown or pnt, culites supremus, Ctenodonta, and

a Cup-coral.

This bed is the lowest in position of the strata here examined ; and,
being tilted up as shown in Section No. 1, it forms the summit or
knife-lke ridge of this mountain which separates the barren alpine
plains of the Puno, on the west, from the verdant tropical regions of
the Yungas, to the eastward. On a clear day the line of bedding of
the last-mentioned strata can easily be followed by the eye, up to the
very highest point of the ridge itself, the steep and highly inclined
sides of which prevent the perpetual snow crowning its top from
showing itself as a continuous envelope, and only allowing it to
lodge itself in the hollows, crevices, and offsets formed by the strata,
which, as it were, prop up its summit.

The section across these beds shows also that the valley of Millepaya
is merely due to erosion, and not to a fault or break in the stratifi-
cation as its peculiar configuration might lead us at first to suspect;
it becomes gradually narrower as it ascends, and loses itself as a
ravine in the western slope of Ilampu. The following observations
of strike and dip were taken :—Bed No. 2: Brown micaceous slates,
N.5°W.,dip 50°W. Bed No.34: Hard, white, altered slates, N.25°W..,
dip 32° W. Bed No. 35: Hardened brownish-white clay-slate,
N. 10° E., dip 35° W. Other observations gave the same strike ;
but the dip was found respectively to be 25°, 30°, 38°, 42° W.; and
still higher up in this bed the observed strike was N. 10° E., and the
dip 40° W.

In these slates abundant furrows and deep grooves were observed,
sometimes very deep, and running from N. 80° E. to E. & W.; also
veins of spathic iron-ore, arsenical pyrites, and auriferous pyrites ;
veins of mispickel or sulpharsenide of iron were found running
N. 50° E. to N. 60° E., and dipping to S.E. at an angle of 75°, cutting
through and altering the strata.

On the sides of this mountain are also found veins of argentiferous
galena, gold-bearing quartz, and metallic bismuth, the latter some-
times in large masses, occasionally faced, or incrusted on the sides,
with metallic gold, sometimes in crystals. Iron-ore is also abundant*.

About ten miles to the south of Millepaya, on the west slope of
ITampu, at Capara, I found, in the loose blocks of soft blue slate there,
Orthis Aymara, a trilobite (probably Homalonotus), a Cup-coral, and
abundant Annelid-burrows, also a Trilobite (possibly a Calymene)
in hard grauwacke.

Still further to the south, at Umapozo, I found Ctenodonta (Nucula),

* T was informed by M. Villamil of a recent discovery of anthracite-beds in
these strata; but, as yet, I have not received any satisfactory confirmation of the
same.

—

1860. | FORBES—BOLIVIA AND PERU. ail

Orthis Aymara, Orthis (Pl. IV. fig. 15), and Cucullella, all in sandy
shale, and in a soft blue clay-slate, apparently the equivalent of the
uppermost beds of the Millepaya section, the Beyrichia Forbesii, asso-
ciated with an abundant small species of Tentaculites, which appears
to me to be quite different from the Tentaculites supremus and 7’.
Saienzii of the lower beds, both of which attain a length of occasion-
ally more than 2 inches, whereas this small species never appeared
to exceed one quarter of an inch.

Between this last-mentioned place and La Paz, I have not exa-
mined the beds for fossils, and only accidentally met with some An-
nelid-tubes in blue slate, about thirty miles north of that city: the

_ position of these is uncertain.

From La Paz, to the eastward, as far as a short way below Unduavi,
in the Yungas, I was enabled to make the section across the Silu-
rian strata between these places, as shown in Section No 2. This
appears to cut through the whole of this formation, from the upper
beds, which before were met with at Millepaya, down to the Lower
Silurian slates with Bzlobites, a thickness of probably about 15,000
feet.

Starting to the eastward from La Paz, and crossing the. great
diluvial formation, with its imbedded stratum of trachytic tuff, which
in the section is seen to be disturbed and dislocated by several faults,
we come upon the first appearance of solid rock some miles to the east
of Chuquiaguillo, and find it to consist of crumbly and much wea-
thered clay-slate, apparently of considerable thickness, and resting
upon greyish impure sandstone, which at the river of Taxani is
succeeded by an alternating series of shales, slates, and grauwackes
or arenaceous beds, the lowest of these being a blue clay-slate of
considerable thickness*, in which an anticlinal is seen, bringing the
former beds again into sight. I noticed before coming to La Lancha
the occurrence of frequent frictional strize and grooves or furrows,
the bearings of several of which I found to vary from N.N.W. to
N. andS., and to N.N.E. At La Lancha these slates again form
an anticlinal, which from the precipitous sides of this immense ravine
could be accurately delineated ; further up, the clay-slates are very
much contorted in the line of bedding; but towards the summit
they become nearly horizontal, or rather slightly basin-shaped; and
in descending, we have the dip always to the eastward until we come
very close to Unduavi. To the west of the summit I did not find any
fossils; but shortly after commencing the descent, the sandy shales
were full of Annelid-tracks, in such abundance that rarely was a slab
found that was not more or less covered with these burrows and
markings. At the Mina Emma, a vein of argentiferous galena,
running from 20° to 35° EK. of N., and with varied but nearly vertical
dip, is being worked; and there I noticed abundant elongated round
bodies in the slate, which from their configuration, and from having
invariably a hollow tube in the centre, appeared like Orthoceratites :
they were composed chiefly of carbonate of iron.

* On the top of these highly inclined strata is seen a small patch of diluvial
conglomerate, apparently a remnant of the formation further to the west.

58 PROCEEDINGS OF THE GEOLOGICAL society. _—_[ Nov. 21,

The rocks from this mine to Pongo, and from that place down to
Unduayi, consist entirely of more or less arenaceous shales, thin-
bedded and containing frequently indistinct traces of fossil forms.
As seen in the section, these slates are dislocated by three faults, which
faults are filled with metallic matter, and form the veins on which are
worked the mines “‘ Delphina,” “‘ Mercedes” (60° N.E. strike, 85° E.
dip), and “ Pilar,” producing argentiferous galena more or less an-
timonial, for the supply of the furnaces at San Felipe.

In M. D’Orbigny’s map, the greater part of these slates are
coloured as granite; and, according to him, Pongo is situated in the
midst of the granite, which in his map here forms a broad band,
constituting the centre of this range of the Andes. As seen in the
section, no trace of granite visible to me occurs here; and, in fact, no
granite whatever is crossed in the direct line of section from La Paz
to as far east of Unduayi as I examined. The small outburst of
granite seen at Silla Tuncari does not occur in this line; and I have
purposely deviated the section from the direct line in order to show
it. Granite is also met with in the Nevado of Chucura, at Yoja, and
at Takesi (to the south of this section); but it does not form the
continuous band seen on M. D’Orbigny’s map, which appears in
this, as in many other instances, to have been coloured from
imagination*.

The granite of this chain of the Andes shows itself at various
localities, apparently isolated one from another?, and appears to be
of the same age as the auriferous granites of the rest of the world,
with which it is identical in mineralogical and chemical composition,
being composed of white orthoclase, colourless quartz, and black or
white mica, and containing frequently spots of iron-pyrites, which
sometimes, as at Silla Tuneari, stains the granite of a brown colour
from oxidation. The gold in this is found in the quartz, or along
with the pyrites; and it would occasionally, at least, appear that
this rock is more auriferous in proportion as it contains more pyrites.
As the whole of this Silurian formation is eminently auriferous, and
contains everywhere frequent veins of auriferous quartz, usually
associated also with iron-pyrites, a study of the occurrence of these
gold-veins leads me to attribute all such veins to the proximity of
granite, and to regard the veins of quartz, iron-pyrites, &c. as haying
been directly injected from the mass of granite itself. We know
that, during the cooling and solidification of granite, the quartz

* In the map which accompanies this memoir (Pl. I.) the granite is not
separately coloured, on account of its forming here a subordinate part of the
Silurian district. It being difficult to get details into so small a scale, the Devo-
nian and Silurian, along with the granite rocks which disturb them, are coloured

with one tint. I must also confess that, without more data, it would be im-
possible to do otherwise without falling into errors similar to those of M.
D’Orbigny.

+ I must observe that I am not alluding to the great granitic range which
occurs, according to M. Pissis, still further to the east, near Coroico. I, unfor-
tunately, was unable to pursue my section further, from the rainy season having
rendered the rivers impassable: an attempt to ford the river below Unduavi
having resulted in the loss of two animals with all the baggage, made it more
prudent to retrace my steps, however unwillingly, to La Paz.

1860. | FORBES—BOLIVIA AND PERU. 59

present in some is the last mineral element to crystallize and become
solid; it seems probable that, during this cooling, the consequent
expansion due to the crystallization of the constituents has forced
those components (quartz, along with iron-pyrites, gold, &c., which
latter, from their very low fusibility, would remain longest of all in
a fluid state), still fluid, into the fissures of the neighbouring rocks,
and so formed such auriferous quartz-veins, which observation shows
are only developed in the slate-rocks at no very great distance from
granitic eruptions, either visible or such as, though hidden, may
reasonably be inferred to exist. This granite is the same which
is everywhere met with in the diluvium of the eastern plateau, as
large blocks, frequently used as a building-material where solidity is
required*,

Although we do not meet with any actual granite on the direct
line of section without diverging (as I have done in order to show the
granitic outburst of the Silla Tuncari), we find, a little to the west of
Unduavi, these beds broken through by a fault, probably due to this
eruption. The granite has also caused an anticlinal in the strata,
which hitherto, from the summit of the pass, had constantly dipped
to the east, but now become inclined to the westward, and continue
so to San Felipe, near which place, however, after presenting some
contortions in their bedding, they again resume their western dip,
haying at the Angostura, below San Felipe, a strike of about N. 30°
E., with 50° westwardly dip.

At San Felipe the hard sandy shales, of a blue colour and slightly
micaceous, contained frequent Annelid-tracks and -burrows, and a
great number of small nail-shaped bodies like the spines of an Echinus,
also others horn-shaped, with concentric rings, both of which Mr.
Salter attributes to Annelids. Along with these were frequent spe-
cimens of the Cruziana Unduavi (P1.V .fig.7); and I also noticed several
specimens of the Boliwana bipenms (fig. 11). Traces of other fossils
were everywhere frequent, but too indistinct to permit determination.

About half a mile further down the valley, Annelid-tracks were
found in abundance in the hard blue siliceous slate, as well as im-
prints of Cruziana. About one mile further down, the thin-bedded
sandy and highly-indurated rocks were literally covered in all
directions with Annelid-tracks and -burrows, the same nail-headed
bodies previously described, and a variety of other and peculiar
markings. J also found some indistinct specimens of Boliviana Melo-
cactus and Cruziana Cucurbita, and several better ones of Cruziana
Unduavi, which last were found a little lower down the valley.
Ripple-marks are everywhere visible in these beds.

In another valley, called the ‘ Quebrada de Aceromarka,” situated
a little to the south of Unduavi, in similar beds, specimens of the
shapeless Cruziana Cucurbita were found in abundance, in company
with the Boliviana Melocactus, and a single specimen of the Boliviana

* The corinthian columns of the new cathedral at La Paz are hewn out of
this granite, and are most creditable to the architect, especially when it is con-
sidered that the cutting of this hard material has been entirely executed by the
Aymara Indians of the district.

60 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

proboscidea*, with numbers of other still more indistinct fossil im-
pressions.

I have not a doubt that these beds, on careful search, would yield
a rich harvest to the paleontologist ; but I had not time to devote
to more than a very rapid survey of the country f.

The thickness of the Silurian strata seen in this section cannot be
less than 10,000 feet: opposite San Felipe a good section is seen on
the nearly perpendicular face of the mountain called “ Perolani,”
which, by measurement, is 6000 feet above the valley; and, as the
strata in the centre of this mountain are nearly horizontal, the thick-
ness of strata in that place cannot differ much from the totalheight of
the mountain above the level of the valley; and itis not too much to
add 4000 feet for the strata visible both above and below these beds.

The Silurian strata have been disturbed by the following igneous
outbreaks, in succession. Commencing with the most ancient,—

1. Intrusion of the auriferous granite, along with its associated
auriferous, and probably other metallic, veins: in parts it
has metamorphosed very considerable areas of the Silurian
beds.

2. The porphyritic eruptions of Hillabaya, Potosi, Oruro, &c.

3. Protrusion of the metalliferous diorites.

4, Still later trappean dykes, which, I am informed, occur at
several localities; but I have not personally come across
them in Bolivia.

5. Voleanic eruptions near the Lake of Titicaca, &c., breaking
out at the borders of this formation, but which, as far as
I am aware, do not anywhere disturb the main chain of
the Silurian Andes of Bolivia. On inquiry, I found that
this district was exempt from the earthquakes which are so
prevalent. and destructive both in this and the adjacent
Republics.

The metallic veinst which occur in these Silurian strata contain
the following minerals :—

Metallic Gold. Fluor-spar.

a Silver. Selenide of Lead.

is Bismuth. 5 of Cobalt and Lead ?

i Antimony. Sulphuret of Antimony.
Oxide of Iron (magnetic). » of Molybdenum.

SOL bin: , of Silver (Silver-glance).
Tin-enamel. Blende.
Chloride of Silver. Galena.

»» of Lead. Magnetic-pyrites.

* T have to thank Mr. Kroeber, the Director of the San Felipe Mining and
Smelting Company, for his hospitality, and the assistance afforded me in my
search for fossils in this region.

+ Mr. Kroeber informs me of some anthracite-deposits, more like fissures filled
up than true beds, and, according to his description, like some in Shropshire.
This, however, requires confirmation.

+ I refer here to such veins as are not (so far as can be determined by super-
ficial examination) in connexion with the eruption of the metalliferous diorites
previously described as of Post-oolitic age.

1860. | FORBES—-BOLIVIA AND PERU. 61

Iron-pyrites. Fahlerz.
Copper-pyrites. Silver-fahlerz.
Tin-pyrites Zinc-fahlerz.
Sulphuret of Copper and Bismuth ? Wolfram.
Jamesonite. Cale-spar.
Plagionite. Carbonate of Iron.
Zinkenite. 4, of Lead.
Lonchidite. Sulphate of Lead.
Mispickel. Phosphate of Lead.

i (niekeliferous). Arseniophosphate of Lead.
Danaite.

The above enumeration is doubtless far from complete ; but it is
quite sufficient to show at a glance how strikingly the mineralogy of
these older strata differs in its general features from that of the more
recent rocks before described.

I may here notice some rocks which occur on the immediate line
of the Bolivian coast, and which, for the present at least, I class along
with the other metamorphic Silurian strata of this part of the world,
not from being able to prove with certainty that they are of Silurian
age, but because, from their position and their relations to the
newer formations in contact with them, they appear to be only a
continuation of the beds which in Chile form the Silurian series of
the coast.

They are so yery much altered by the effects of the eruptions of
granite, porphyry, and diorite, which here break them up, that even
their sedimentary nature can hardly be recognized except at some
few localities.

To the south, in the Desert of Atacama, they appear as gneissic or
metamorphic schistose rocks, broken through in all directions by
granitic outbursts, the granite itself being precisely identical in
external appearance and mineralogical composition with the pre-
viously described auriferous granite of Silurian age in the Eastern
Andes. It is composed at Mexillones, for example, of white ortho-
clase, colourless quartz, and dark mica. Further southward the
sands arising from the disintegration of this granite have been proved
to be auriferous.

At Cobija, the black rock which forms the rugged low cliffs and
detached rocks in the sea and along the shore appears also to belong
to this series, although in appearance it frequently resembles a com-
pact trappean rock or a black porphyry. On closer examination, I
am disposed to consider it as a clay-slate or other argillaceous or
calcareo-argillaceous rock, fused im situ by the action of the masses
of porphyry or diorite resting immediately upon it, or of the granite
which has upheaved and broken it up, and which, although not
itself visible at the Port of Cobija, is seen a little further to the
south. This rock varies in colour from a bluish-grey to grey or
bluish-black, and, like all altered rocks of this class, contains
green epidote frequently disseminated in it, or forming imbedded
geodes: geodes of quartz or calcedony also occur; and when the
rock appears to have been completely fused I have noticed some dark-

62 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

grey felspar-like mineral in it; in texture it then much resem-
bles a basaltic or trappean rock. It is extremely hard and tough,
and is cracked, fissured, and jointed in all directions. Occasionally
one set of joints presents pretty regular and parallel lines of fracture.
Many small strings of copper-ores (sulphurets, carbonates, and oxy-
chlorides) are seen cutting through them, with various bearings, from
N.E. to E. and W., dipping at very high angles.

Conclusion.—In conclusion, I must direct attention to the three
comparative sections of the country from Arica on the Pacific to the
Yungas on the eastern side of the High Andes of Bolivia (Plate I11.).
Although this plate is, of cowrse, to be regarded only as a diagram, it
represents correctly a summary of the conclusions at which M. D’Or-
bigny*, M. Pissist, and myself have arrived in traversing the same
line of country.

On examination, it will be observed that great and unaccountable
differences are here depicted ; and it must be left to the reader to
judge, from the perusal of the different memoirs of the three authors,
how far each of them may be sound in his views.

This plate does not require any further explanation than the
remarks which have been occasionally made under the heads of the
different formations ; but it is particularly important as showing at a
glance these several discrepancies, and in its bearings on the general
tenor of the results here brought forward. Subsequently it will be
required for reference in the second and third parts of the memoir of
which this communication is the first part, and which will treat of
the Geology of Chile and the Argentine Provinces ; it will then be
found most essential in explaining and reconciling the various state-
ments which have been made in reference to the geology of these
countries.

2. On the Fossits, from the Hieu Anpzs, collected by Davin Forszs,
Esq., F.R.S., F.G.8. By J. W. Satter, Esq., F.G.S.

[Puaves IV. & V.]

J HAVE examined this unique series with some care; and with a col-
lection of above 200 specimens there should be no unusual difficulty
in assigning the true geological date. The specimens are generally
perfect enough to show the generic characters, though in very few
cases is their preservation complete; and it is thought better at pre-
sent (especially as Mr. Forbes intends returning over this difficult
ground) to figure all the chief forms, and give specific characters
only to the more prominent fossils. All the specimens from the
slate-rocks are distinct from those previously published.

* Voyage dans |’ Amérique Méridionale, tome iii., Partie Géologie. Par M.
Alcide d’Orbigny. Paris, 1842.

t “Recherches sur les Systémes de Soulévement de l’Amérique du Sud.” Par
M. Pissis. Annales des Mines, 5™ sér. tome ix. 1856. “

Quart. Journ. Geol. Soc. Vol: XVII. PI: 1

A 65?

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of part. of

BOLIVIA anp PERU
By D.Forbes, FRS. EGS, &.
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Diwvisl = EER.
Carboniterous
(Co bitinles Skat «

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Section

Chipicani. 197407

hardened sandstones.
Quartz feolourtess) &

Gramvacke & impure
Mica (black!

Shales and slates,

Silurian.
In generat.
&
Orthaclase /white/,

Devonian.
Gr anit e (Middle Silurian)

-stones, marls, & clays,

Red. and yellow sand -
“Carboniferous.

Tn general.

Altered: Rocks.
Gypeunbeds andi
Copper-saridstones.
Shales and. slates.
Grits and sandstone.

Permian.

i
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Cuylonese::

0

Y

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tied:

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» Upper Oolitic.

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debris:

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ratiwod:

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320 mtles.

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1860. | SALTER—BOLIVIAN FOSSILS, 63

Of the Carboniferous forms little need be said. They are the same
as those described long ago in D’Orbigny’s large work; and similar
specimens were brought home by Mr. J. Cumming during his ex-
plorations for recent shells in Bolivia. The resemblance to British
fossils of this epoch is most striking, and some of the species are
identical.

The Devonian gives us very scanty traces, yet scarcely doubtful.
Occurring, as it does, between the Carboniferous basin and the slate-
rocks, it falls naturally into the place indicated by the few fossils
known tous. Mr. Pentland brought home from Aygatchi, in Bolivia,
a Trilobite from this formation.

The age of the slate-rocks, however, was for a long time doubt-
ful; and the aspect of Mr. Forbes’s collection is so unlike that of
any British or American type, that, while their discoverer was
strongly urging their Silurian age, my own prejudice gave them
a Lower Devonian character. The large Homalonoti (the only con-
spicuous Trilobites) are, on the whole, more like Devonian forms
than Silurian; and the shells are of just such types as might be
referred to either of these systems. The Tentaculites would bear the
same interpretation ; but a small Beyrichia, very rare, occurs just at
the top of the whole series, and this particular form of the genus is
not known in Europe to trespass beyond the Uppermost Silurian
limit, or the basement-beds of the Devonian at furthest. Again,
the Bilobites (whatever these obscure fossils may be) are all of
Silurian age, and they are numerous in Mr. Forbes’s collection.
They have generally been regarded as Lower Silurian forms, and
are, indeed, far more plentiful below the Caradoc rocks than else-
where. But too much stress must not be laid on this; for one cha-
racteristic species occurs in the Llandovery or Clinton group of New
York; moreover, all the specimens from the Andes, whether the
large ones described by D’Orbigny, or the smaller ones now brought
home, are of species distinct from those known in other districts.
I do not believe them to be plants, but have no definite idea of their
true structure, further than that they were tough hollow crusts, not
soft solid masses as sea-weeds generally are.

One other remark before proceeding to notice the separate species.
Wherever we meet with new areas of Silurian rocks, we find we have
in them new Natural-history provinces of these old seas: it is so in
India, according to Colonel Strachey’s researches ; and it is so in Au-
stralia : no species from either region is, I believe, identical with those
of Europe. The same cannot be said of the Devonian fossils, which
ranged very widely during the later part of that epoch; and the
Carboniferous types are almost cosmopolitan, many of the same
fossils ranging from the North Pole to Australia, and from North
America and the Andes to Nepaul. It is, I think, chiefly due to
this circumstance that we have been accustomed to regard the
Paleozoic types as having an almost universal diffusion. This is
nearly true as regards the genera, but, except in the remarkable
case of the Mountain-limestone fossils, without much evidence in
the case of species.

64 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21, ©

CARBONIFEROUS.

From the small basin of these rocks at the Isthmus of Copacabana,
in the Lake of Titicaca, the following species were obtained :—

Productus semwreticulatus, Martin. (P. Inca, D’Orb.) PI. IV. fig. 1.
Longispina, Sow. (P. Eee DOxrb.) < RIVE ie

Spirifer Condor, D’Orb. (Sp. striatus, Sow. ?)

Bolwiensis, D’Orb.

Orthis resupinata, Sow. ?

Andi, D’Orb. (from a Santa Cruz specimen). PI. IV. fig. 3.

Athyris subtilita, Hall. (Ter. Perwiana, D’Orb.) Pl. IV. fig. 4.

Rhynchonella (a species with three raised ribs, very like some va-
rieties of &. Plewrodon ; also from a good Santa Cruz specimen).
Teds 1A atte f5¥

Euomphalus, with separated whorls (possibly a Phanerotinus).

Bellerophon, sp. ; a close ally of B. Uri, Flem. PI. IV. fig. 6.

Corals, also, and Crinoids, all imperfect. D’Orbigny describes a
Favosites and a Cup-coral, a Fenestella, &e.; and Col. Lloyd’s col-
lection from Arque, as well as Mr. Cumming’s from Santa Cruz, both
include such specimens. I see no essential difference between the
Productus semireticulatus, so common in Britain, and the so-called
P. Inca of D’Orbigny ; and I think it would puzzle any one to draw
a clear distinction between his P. Capacii and our own familiar
P. Longispina, found everywhere in the Carboniferous Limestone.
The Spirifer Condor has certainly rougher ribs than the ordinary
varieties of Spirifer striatus, and may be distinct. We figure (Pl. IV.
fig. 3) one remarkable form, said to be from Santa Cruz, but, at all
events, from the Carboniferous Limestone of the Andes, of which less
perfect specimens occur in Mr. Forbes’s collection. It is a beau-
tiful species of the Orthis resupimata group, and has received the

absurd name of O. Andi from D’Orbigny.

Our figure of the Rhynchonella (Pl. IV. fig. 5) is also from this
collection, which was sent home by Col. Lloyd many years back.

DEVONIAN*.

Ortuais sp.) BIPRY). fies /-

Internal casts only. It belongs to the group of Orthis resupinata
and O. Michelini, and thus may be either Carboniferous or Devonian.

Locality. Oruro. Sent from thence by Col. Lloyd. (Mus. Prac-
tical Geology.)

* Of the seven species considered Devonian by D’Orbigny, only’ four appear
to be certainly supra-Silurian ; and these four may (from their type) be either
Devonian or Carboniferous. They are—Rhynchonella Peruviana, Spirifer Boli-
viensis, S. Quichua, and Orthis Inca. Spirifer Quichua is from Chuquisaca, the
other three from Cochabamba.

The Orthis pectinata, on which D’Orbigny lays stress, seems to me to be very
unsatisfactory. It is only the cast of a single valve, without hinge or teeth, of a
shell destitute of any marked characteristics. I should not like to speculate as
to its age; but M. D’Orbigny may have seen Devonian species like it.

1860.] SALTER—BOLIVIAN FOSSILS. 65

Puacops LAtirrons, Bronn. (P. Bufo, Green.) Pl. LY. fig. 8.

In all essential particulars this agrees with the common Devonian
species known in Europe under the name P. latifrons, and in America
by Dr. Green’s appellation P. Bufo. Comparing it with either
Spanish or American specimens, I see no difference, except a some-
what flatter axis, and perhaps one rib fewer in the tail-piece. The
group of Phacops to which it belongs sometimes occurs in Upper
Silurian strata; but this species is nevertheless a most characteristic
Devonian form, and has an immense geographical range.

Locality. Near Oruro. In a rolled pebble.

Mr. Pentland found near the town of Aygatchi, Bolivia, another
Phacops, which, from its type, belongs most certainly to Devonian
rocks. It is one of the group Crypheus, distinguished by having
the border of the tail spinose; moreover, it is not far removed in
affinity from the characteristic Phacops Caffer and P. Africanus of
the Cape of Good Hope. P. (Calymene) Vernewlit of D’Orbigny
appears to belong to the same section, and is probably of the same
age.

Puacops (Crypumus) Panrnanptr, n. sp. Pl. IV. fig. 9.

Rather more than 2 inches long, and 1+ inch broad, convex,
long-ovate, with a subtriangular head; the tail pointed, ribbed
throughout, and with a tubercular or subspinose border,

Head ? inch long, blunt-trigonal; the glabella broad, inflated in
front, the forehead-lobe rhomboidal and blunt-pointed, but not over-
hanging; the facial suture supra-marginal. The margin itself is
thin in front, thickened only round the sunken cheeks, and is cut near
its (spimose ?) posterior angle by the facial suture. Eye prominent, of
many moderate-sized lenses, set far forward, but not close to the
glabella.

Body-rings (much broken) with the axis very prominent, and with
four spies on each ring, besides one within the fulerum on the
pleura, and one (or two?) outside it; pleural groove deep, broad ;
ends of pleure truncate.

Tail-piece triangular, 6 lines in length, wider than long, with a
very convex axis reaching the tip, and marked by six or seven strong
rings, the rest indistinct. The sides are about the same width as
the axis, with six strong curved ribs (the upper ones duplicate), not
furrowing the narrow border, but faintly continued on it into mar-
ginal tubercles. Both the lateral ribs and the axis have tubercles
on them. The terminal spine, if one existed, is broken off.

There are several Bohemian species of Phacops which resemble
this in the tubercular ornaments of the body; but none that I know
haye a tuberculato-spinose border to the tail; and this character,
combined with the inflated forehead-lobe, will certainly restrict the
fossil to either Upper Silurian or Devonian: it cannot be Carboni-
ferous.

Locality. Aygatchi (Mr. Pentland, 1827). It comes, according to
that gentleman, from beds of the Carboniferous series; it would ap-

VoL. XVII.—PART I. F

66 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

pear from Mr. Forbes’s statements, that it could only be from the
sandstones at their very base; and I must claim these as Upper
Devonian.

Favosrres(?), sp. Pl. IV. fig. 10.

I find no pores in any of the tubes (but only some tubercles), and
very few traces of tabule. Possibly it is not of this genus.

Locality. Given to Mr. Forbes (by Mr. Bogen, of Tacna) as haying
been found near Oruro.

UPPER SILURIAN.

All the thick beds of sandstone, intercalated with many layers of
sandy shale, appear to lie in the upper part, or middle part at least, of
Mr. Forbes’s Silurian section ; and in these the chief part of his fossils
were found. The lower beds (chiefly shale and thin sandstones)
contain the Bilobites (or Cruziana) and very little else; and, seeing
that his sections gave a measured thickness of at least 15,000 feet
(all of which, as he judges by the mineral aspect, belongs to one and
the same series), there is much reason for supposing the lower part
to be of Lower Silurian date. This is borne out by the presence of
the Bilobites, which, as above noted, is chiefly a Lower Silurian type.

D’Orbigny has figured a Graptolite, with one row of cells, from
South America; and this alone would prove the presence of Silurian
rocks, upper or lower. It is from Tacopaya, Santa Cruz.

Homatonotus Linares, n. sp. Pl. V. figs. 1 & 2.

Body (?) faintly trilobed (fig. 1 @); pygidium (fig. 16) 14 inch long,
and about as broad, triangular, regularly convex, with the sides not
abruptly bent down. ‘The axis is but faintly marked, quite as broad
as the sides, and scored by about sixteen rings; the sides show
nearly as many furrows, none of which reach the margin. The apex
is pointed, the tail gradually tapering to it, not abruptly acuminate.
The sides (apparently from fig. 16) are bent inwards beneath; and
the apex also shows some indications of a broadish triangular space.
The whole surface appears smooth.

The species is not unlike H. delphinocephalus, Murch., but has
many more ribs, and a longer axis.

Locality. From the highest point reached by its discoverer: he
found it on the all but imaccessible face of Mount Iampu, at the
height of 20,000 feet. Named in honour of his Excellency the
President of Bolivia.

Homatonorts, sp. Pl. V. fig. 3.

Not perfect enough to describe. It has a blunt rounded shape,
like that of H. obtusus, Sandberger, and several other German and
French speciés from Devonian rocks. The axis is more strongly
ribbed than the sides, and the surface is roughly granular.

Locality. From the same mountain as above, at a somewhat lower
level (about 15,000 feet).

1860. ] SALTER—BOLIVIAN FOSSILS. 67

PRoEtTvs, sp. (a fragment). Such fragments are common both in
Upper Silurian and Devonian rocks.
Locality. Same mountain (16,000 feet).

[Bryricuia Forsusrt, Jones, n. sp. Pl. IV. fig. 15 a, 6, c, nat. size
and magnified,

Carapace-valves oblong-ovate ; straight on the dorsal and obliquely
curved on the ventral edge ; obtusely tapering at one end, obliquely
truncate at the other; bordered below and atthe ends with a slight
rim: surface raised into four, equidistant, unequal, transverse,
rounded ridges; the one next to the narrow end of the valve lowest
and shortest, the next one highest and longest of all.

This is nearly allied to Beyrichia Bussacensis from the Lower
Silurian rocks of Portugal (Quart. Journ. Geol. Soe. vol. ix. pp. 141,
160, pl. 7. figs. 5 & 6); but it is narrower, and its ridges are
differently proportioned. It also approaches in form to the figure of
a Beyrichia that has been published (without description) by Prof
KE. Emmons among some Silurian Fossils of North America in his
‘ Manual of Geology,’ 2nd edit. 1860, p. 100, fig. 90.

This little fossil is seen in some numbers (together with Tentacu-
lites) on a small piece of dark-grey calcareous schist from the
western slope of [lampu in the Bolivian Andes. It is dedicated to
its adventurous discoverer, Mr. David Forbes.—T. R. J.]

TENTACULITES SUPREMUS, n. sp. PI. IY. fig. 11.

Nearly an inch long, diameter 2 lines, cylindrical, slowly tapering
until near the apex; marked at intervals of about a line by cord-like
ridges, strongly projecting, and often in pairs. Between these are
close concentric annuli, or fine ridges, about thirteen in the space of
a line.

The strong double ridges which ornament this species occur chiefly
on specimens which have the rings more distant than others. They
remind one much of the Yentaculites in the Wenlock strata of the
Isle of Gothland. I believe this species to be a new one; it is a
good deal like 7. ornatus, Sow.

Locality. On the snowy ridge of Ilampu, in company with Ho-
malonotus Linares. A Ctenodonta and a Cup-coral are found with
them.

Tentacurires Sarenzi, nu. sp. PI. IV. fig. 12.

Tapering more rapidly than the last, and marked by numerous
equidistant rounded rings [with no intermediate annuli?]. The
want of annular strie may be only a comparative character ; but the
regularity of the somewhat oblique rings seems to be specific,

Locality. It occurs in the grey shaly beds between the grits of
Tlampu, and is dedicated (by Mr. Forbes’s request) to Senor Saienz,
whose kind and efficient help was of great service to him in his
explorations.

Smaller Tentaculites (fig. 13 a) occur in some of the slabs with the

R2

68 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

Beyrichia above noticed; but they are probably the young of one of
the foregoing species.

In Europe the strata in which Zentaculites are conspicuous are—
Caradoc Sandstone, Llandovery rock, and Lower Devonian. In North
America (New York) they appear to be more specially confined to
the Devonian strata. They are known all over the world in Paleo-
zolc rocks.

Burrows and Casts of Marine Worms.

Such impressions as these attract the attention of every close
observer. The peculiar habits of marine worms, introducing, as
they do, the sabulous matter from one stratum into the more clayey
beds of another, have a special tendency to render the rock compact
and tough-bedded. Mr. Forbes found the worm-markings of all sizes,
both in the upper and lower beds of the Silurian rocks, and either
as double burrows, single vermicular casts, or in groups, just as we
find them in our own Ludlow, Devonian, and Carboniferous strata.

Ortuis Aymara, n.sp. PI. IV. fig. 14.

Variety (?) of Atrypa palmata, Morris and Sharpe, Quart. Journ.
Geol. Soc. vol. 1. pl. 10. fig. 3: Orthis palmata, Sharpe, Trans.
Geol. Soc. 2 ser. vol. vi. p. 207.

Cireular, or only slightly transverse, strongly ribbed, with a very
short, almost obsolete hinge-line; ventral valve convex, gibbous
near the beak, with a depressed central rib near the margin; upper
or dorsal valve flat, with two slightly raised ribs in the middle ;
ribs about 14, acute, no intermediate ones. Diameter about half
an inch.

The above may stand as the obvious characters of this abundant
species. As distinguished from the common southern form above
quoted, the size is less, and the ribs not quite so prominent; but the
chief difference is in the interior, which shows (in O. palmata) very
strong dorsal teeth, and the ventral hinge-plates thick and short.
Ours has but thin plates, and moderate-sized teeth.

I hardly see sufficient reason for considering O. Aymara a distinct
form. It is very similar to the common African species above
quoted, which also occurs at the Falkland Islands. The same fossil
appears also to be frequent in the Lower Devonian rocks of Gaspé,
Canada. But these localities being all Devonian, one is scarcely
justified in uniting with these the Silurian shell from the Andes, if
there be any structural differences. Orthis palmata is evidently a
common shell; and such species have, as Edw. Forbes first showed,
a wide range in time as well as geographically: Atrypa reticularis
is a case in point, ranging, as it does, from the Middle Silurian to
the Upper Devonian, and as a frequent shell throughout. The
O. Aymara may, very probably, when we have more specimens,
turn out to be the Silurian variety of a shell which attained a fuller
development in Devonian times as O. palmata.

Localities. Valley of Millepaya, and other localities on the western
side of the Andes.

1860. | SALTER—BOLIVIAN FOSSILS, 69

[The Aymara Indians are supposed to have been the original
inhabitants of these mountains. They still linger there, having
never been completely conquered, and never having amalgamated
with the Quichua or Inca race.—D. F.]

Orruis, sp. PI. IV. figs. 15 & 16.

A small Orthis, which may be equally compared with varieties
of the O. elegartula, Dalm., or with the Devonian forms, O. opercu-
laris, &c., from the Eifel. The strie seem to be pretty regularly
interlined with smaller ones. In the absence of more perfect spe-
cimens, I do not give ita name. It is certainly not a young spe-
cimen of the O. Humboldtiz of D’Orbigny.

Locality. Valley of Millepaya, and further south on the western
slope of Iampu.

STROPHOMENA, sp.

A mere fragment or two of a small thin-shelled species, with fine
radiating strie.
Locality. Cotana, about five miles south of the town of Sorata.

CucvLtELia, sp. Pl. IV. fig. 17.

The transverse, oval and convex form of this shell reminds us of
C. ovata, Sow., rather than C. antiqua of the same author. Both
are Ludlow Rock species: but there are Lower Devonian forms very
like them both in Britain and South Africa. The muscular plate ex-
tends, vertically, two-thirds across the shell.

Locality. West face of Illampu.

Crenoponta (Nucuta), sp. Pl. LV. fig. 18.

This is figured, because it is rather common. Such transverse
forms, concentrically striate, and a little antiquated in the lines of
growth, are knownin all Paleozoic formations.

Locality. Valley of Millepaya; also further south, on the western
slope of Illampu.

Axrca ? Brownit, sp. Pl. IV. figs. 19 & 20.

Broad-oval, more than 24 inches wide, and 12 deep; the beak
at the anterior fourth not very prominent, the hinge-line tolerably
straight, not curved down. The posterior side is nearly as broad as
the depth of the shell beneath the beak, slightly angulated along
the posterior slope, and rounded at the posterior angle. The an-
terlor side is somewhat produced, and straight along its hinge-
margin. Surface marked by rather distant lines of growth, and
covered all over the central parts of the disk by fine radiating strie,
sharply impressed, very unequal in size and depth, wavy in their
course to the margin, and interlined by lesser ones. They are
altogether absent on the anterior and posterior fourth. On our
large specimen this effacement of the strie is gradual; but in some
others it is sudden, and the central striated area in these specimens
is sunk below the general surface. These may be of a distinct species.

J

70 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Nov. 21,

Fig. 20 represents a young specimen. ‘The outline is much more
rounded, however, if that be not due to pressure; and the duplicated
striee cover all the surface.

Locality. West slope of Tllampu. [Fieldmarshal Brown, a well-
known general of the War of Independence, and after whom this
shell is named, showed much interest in these researches, and was of
great assistance to the author of the foregoing memoir.—D., F.]

BELLEROPHON, sp.

About 1 inch wide, having a large body-whorl, a small spire, and
the whorls not at all involute; umbilicus quite open, and the
whorls sloping towards it. Striz of growth arched backwards to
the carinate margin, which, however, is obtuse, not sharp-edged.

Locality. Common enough in some hand-specimens from the west
side of Ilampu.

Pareria or Preeorsis ?

An extraordinary specimen of a suboyate clypeiform shell, an inch
and.a half in its largest diameter, and rather more than an inch
wide, has an excentric blunt umbo, and a rather wavy margin. The
surface is covered with close concentric ridges, which show equally
well on the external and internal cast. ‘The general appearance is
that of an oblique Patella, or rather one of the Calyptraide. But it
is too imperfect to decide upon. Patelliform shells are known in the
Silurian, but they are very rare.

Locality. West side of the Valley of Millepaya.

LOWER ? SILURIAN.
Crozrana, D’Orbigny.

It seems hardly worth while to separate these obscure fossils into
several genera while we know so litle of them; but certainly
they cannot all belong to one group. The distinctly grooved and
bilobed form, which induced M. Cordier to apply the name Bilobites
to them, is characteristic of the species described by D’Orbigny,
and of some others foundin N. America. The more elongate strap-
shaped species found in Europe have already received names from
M. Rouault in his memoirs on the Silurian Rocks of France. And
the species here figured belong to such various plans of form that,
if we only knew a little of the nature of the bodies in question, we
should be bound to give them separate names; at present I only
propose one for the sagittate forms—Boliviana. Mr. Forbes did
not meet with either of D’Orbigny’s species, which, from that au-
thor’s description, came from Lower Silurian beds*, Those here
described are also the lowest fossils in the section.

* “C'est le premier corps organisé qui se montre au-dessus des phyllades
schistoides, dans les phyllades micacés brunatres.”—Voyage, &c. vol. ili. part 4
(Paléontologie), p.31. Mr. Forbes thinks, however, that there is no evidence of
their being so low in the series.

1860. ] SALTER——BOLIVIAN FOSSILS. wil

Cruziana Cucursita, n.sp. Pl. V. figs. 4, 5, & 6.

Three inches long, elongate, clavate, curved into a shape more or
less sigmoid, subcylindrical in section, compressed; rounded at the
anterior end, tapering posteriorly ; smooth, except a few irregular
wrinkles, but with a raised longitudinal rib throughout (down each
side ?).

I a not sure whether the raised rib which runs from end to end
of these shapeless masses is an external marking, or arises from an
internal hard cylinder. Fig. 6 shows some irregular transverse
wrinkles ; but, except these, there is no marking whatever to distin-
guish this form, which may be recognized by its blunt clavate shape,
like many of the gourd-fruits, whence the name.

Locality. Very plentiful on the surfaces of grey schist. Valleys
of Unduayi and Aceromarka.

Cruziana Unpuavi, n.sp. Pl. V. figs. 7 & 8.

Three or four inches long, subcylindrical, but often flexuous,
slowly tapering. Surface marked with numerous (9 or 10) longi-
tudinal ribs, which run for short distances only, and alternate,
leaving some parts smooth. The general direction of the ribs is
longitudinal, but wavy.

Localities. Valleys of Aceromarka and Unduavi, where it is most
abundant.

BoxivIaANa, gen. nov.

Form obcordate or sagittate, tuberculate or ridged, without a
central furrow, and produced behind into two barbs or wing-like
appendages. (A peduncle or stem occurs in some species.)

These broad arrow-shaped forms differ so much from the true
Cruziana, that it does not seem premature to separate them. (I
leave the elongate forms at present all in one genus.) And the
general term Bilobites may still be conveniently used for the whole
group, though not now accepted as a generic term.

Borrviana Metocactus. Pl. V. fig. 9.

Three-quarters of an inch long, obcordate, deeply notched behind,
and pointed and produced backward on each side. Surface gently
convex, rising into a ridge along the median line, which projects
a little in the middle of the deeply emarginate posterior edge. Six
longitudinal ridges, narrower than the central one, run along the
whole length, with irregular tubercles on them, arranged so as to
form tranverse rows, seven or eight on each side.

A rough resemblance to the mammillated plants so common in
the region of the Andes suggests the name.

Locality. Valley of Aceromarka, north-eastern slope of Illimani.

BoLtvIANA PROBOSCIDEA. PI, Y. fig. 10.

This appears to be only about half of the disk, and it is therefore
described as if the longitudinal ridge (a) were central. An inch
and a half long, narrow-sagittate, lanceolate, convex; with a very

72 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

prominent central ridge, produced behind into a thick blunt spine.
Posterior edge doubly emarginate, but with the angles scarcely at
all produced. Six longitudinal ribs on each side of the central one,
all closely tuberculate, so as to form transverse rows.

The projecting mass is supposed to be the stem, and is nearly as
long as the frond, very thick, obtuse, attached to the posterior mar-
gin, and shaped like the siphon-sheath of a bivalve shell.

Locality. Valley of Aceromarka.

Borrviana BrPennis. PI. V. fig. 11.

Mr. Forbes observed the other part of this specimen in the rock,
but could only detach one half. ‘The outline is therefore added to
our figure.

Frond semioval, emarginate behind, gibbous at the sides, and
with the posterior angles produced into strong divergent tapering
spines. Surface marked by ridges and furrows parallel to the
curve of the front and back margins. Spines also furrowed near
the base. Stem (apparently attached) long filiform.

Locality. Valley of Unduavi, eastern slope of the Andes.

Summary.

The number of species that we recognize in this collection, made
with so much perseverance and at great personal hazard, are—
5 Lower? Silurian (Bilobite-schists).
14 Upper Silurian (grey sandy schists and sandstones).
3 Devonian.
13 Carboniferous.

D’Orbigny’s collection of Silurian fossils contained 10 species, of
which none have occurred to Mr. Forbes. They are—

Cruziana rugosa. Phacops (Calymene) Verneuilii.
furcifera. (C.) macrophthalma ?

Orthis Humboldtii. Asaphus Boliviensis.

Lingula marginata. —
Muensterii. There is some doubt about both his
dubia. species of Phacops. They are probably

Graptolites dentatus. Devonian.

Adding these to our list, we obtain 27 or 29 Silurian species for the
Central Andes, belonging to a fauna specifically different from that
of any other quarter of the world. I venture without hesitation to
assert that the identifications by D’Orbigny with European forms,
where I am acquainted with the species, are wrong. I am obliged
to say this much, since that distinguished author has fearlessly
united things which differ by the most obyious external characters,
and has lent the sanction of his great reputation, on such evidence
as this, to a former community of species, and an equable diffusion of
heat. In regard to the Carboniferous forms, where M. D’Orbigny
is unwilling to allow more than a close analogy between the two
continents, | am again compelled to differ from him, but it is in
an opposite direction.

Gnart. Journ. Geol.Soe Vol XVITPLLY.
CARBONIFEROUS.

Ps 7 Bile
rt

FOSSILS from the ANDES.

ee
ne

Quart. Journ, Geol. Soe Vol.XVIL PL V.
Ea Ts UPPER SILURIAN.

SILURIAN.

SILS from

GB. Sowerky.

1860. } HUXLBY—MACRAUCHENIA BOLIVIENSIS. 73

EXPLANATION OF PLATES IV. & V.

Tilustrating Mr. Salter’s paper on some Palzozoic Fossils from the Bolivian Andes.

Prats IV.

. Productus semireticulatus, Martin. Isthmus of Copacabana.
P. Longispina, Sow. Isthmus of Copacabana.

Orthis Andii, D’ Orb. Santa Cruz.

Athyris subtilita, Hal/. Isthmus of Copacabana.
Rhynchonella, sp. Santa Cruz.

. Bellerophon; like B§Urz, Fleming. Isthmus of Copacabana.
. Orthis, sp. Oruro.

. Phacops latifrons, Bronn. Oruro.

. Ph. Pentlandii, Salter. Aygatchi.

10. Favosites (?), sp. Oruro.

11. Tentaculites supremus, Salter.

12. T. Saienzii, Salter.

13a. Tentaculites, sp., and Beyrichia Forbesii, Joncs.
136 &13¢. Beyrichia Forbesii, Jones.

14. Orthis Aymara, Salter. :

15, 16. Oakes , 8p. | Valley of Millepaya.

17. Cucullella, sp. Illampu.

18. Ctenodonta (Nucula), sp. Valley of Millepaya.

19. Arca (?) Browniu, Salter. Fig. 20. Young specimen. Illampu.

Fig.

Co HATH OU CO LO EH

Illampu.

Puate V.
Fig. 1 & 2. Homalonotus Linares, Salter.

3. Homalonotus, sp. Ilampu.

4, 5, & 6. Cruziana Cucurbita, Salter. ‘

7&8. C. Unduavi, Salzer.

9. Boliviana Melocactus, Salter. Valleys of Accromarka and
10. B. proboscidea, Salter. Unduavi.

11. B. bipennis, Salter.

3. On a New Species of Macravcuenta (M. Boliviensis). By
THomas H. Huxtry, F.R.S., Sec.G.8., Professor of Natural
History, Government School of Mines.

{PuaTe VI.]

Tue vertebrate remains obtained by David Forbes, Esq., F.R.S.,
F.G.S., from the mines at Corocoro, under the circumstances de-
tailed in his paper “‘ On the Geology of Bolivia and Southern Peru,”
consist of the following parts of the skeleton of apparently one and
the same Mammal:—1. A portion of the right maxilla and palate,
with fragments of grinding teeth. 2. Rather more than the right
half of the occipital portion of the skull. 3. A middle cervical ver-
tebra, nearly entire. 4. A fragment of a posterior lumbar vertebra.
5. A small portion of a right scapula. 6. A crushed fragment of the
proximal end of anulna. 7. Part of the proximal end of the left
tibia. 8. The entire left astragalus, and part of the right astragalus.

74 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 21,

The bones are all in the same, and that a very peculiar, mineral
condition—the Haversian canals being for the most part filled up
with threads of native copper; so that the fossils are not only ex-
ceedingly dense, but, in consequence of their internal flexible me-
tallic support, their thinner and more delicate parts bend, rather than
break, when force is applied to them.

The characters of the cervical vertebra and of the astragalus, which
are fortunately the best-preserved of all the fossils, at once demon-
strated the remains to belong to the genus Macrauchema (Owen),
while the entire absence of epiphysial sutures in the vertebre and
the long bones, and of similar indications of immaturity in the frag-
ment of the skull, proved the animal to have attained its adult con-
dition. The vertebra and the astragalus, however, have not more
than half the size of the corresponding bones of the species, J. Pa-
tachonica, discovered by Mr. Darwin, and described by Professor Owen
in the ‘ Appendix to the Voyage of the Beagle’; and as, in addition,
these and the other bones present different proportions from those of
the Patagonian species, I have no hesitation in regarding the fossils
collected by Mr. Forbes as the remains of a distinct species, for which
I propose the name of Macrauchenia Boliviensis. It will be con-
venient to commence the description of these fossils with those parts
upon which the diagnosis of the species may be most safely rested,
viz. the cervical vertebra and the astragalus.

The cervical vertebra (Plate VI. fig. 1).—The great length of the
centrum of this vertebra, the peculiar form of its transverse processes,
and the absence of perforations for the vertebral arteries in them
are characters which, in the present state of knowledge, oblige the
anatomist at once to refer it either to one of the existing Camelide
or to the genus Macrauchenia; while the two strong, converging
ridges which mark the posterior half of the under surface of the ver-
tebra, and meet to form a single ridge, which dies away anteriorly in
the middle of that surface, togetherwith the shght concavity of both the
posterior and the anterior articular faces of the centrum, are decisive
in favour of the latter alternative. In fact, the excellent description
of the cervical vertebre of Macrauchenia Patachonica which has been
given by Professor Owen applies so well to that of I. Boliviensis,
that, referring to the paper in the ‘ Appendix to the Voyage of the
Beagle, already cited, for a general account of the characters of
Macrauchenian vertebra, I shall content myself with pointing out
the resemblances and differences of the Bolivian from the Patagonian
Macrauchenia, and from the existing Aucheniw. The dimensions of
the centrum of the cervical vertebrae of the two Macrauchene, and
of the fourth cervical of a Guanaco and of a Vicugna in the College of
Surgeons’ Museum are as follows :—

M. Boliviensis. M. Patachonica. Guanaco. Vicugna.

in. in. in. in.
Men oth... Heese 3°8 6:6 4-6 4:0
Width of anterior face 1:1 32 11 8
Width of posterior face 1:25 34 13 1:0

1860. ] HUXLEY—MACRAUCHENIA BOLIVIENSIS. 75

Thus it appears that the centrum of the cervical vertebra of
Macrauchenia Boliviensis is far more slender than that of M. Pata-
chonica; for, while the length of the former is to that of the latter
as 1; te the transverse diameters of the anterior faces of the centra
of the two species are, nearly, as 1:3. The cervical vertebra of the new
species 1s, absolutely, rather shorter than the fourth cervical of the
Vicuena ; but, relatively to its width, it is much shorter and stouter
than this bone in either the Guanaco or the Vicugna. There are no
longitudinal ridges on the surface of the vertebra below the pre-
zygapophyses, in which respect M. Boliviensis differs from M. Pata-
chonica, and approaches the Auchenie. The anterior articular facet
of the centrum is concave from above downwards, in consequence of
the projection of the thickened and convex lower third of that face ;
the posterior facet is not only concave from above downwards from
a similar cause, but is also concave from side to side, The con-
cavity of both articular facets is greater than in M/. Patachonca,
and the present species departs, in these respects, more widely than
the latter does from the Auchenie.

The astragalus (Plate VI. fig. 2).—This bone is, again, quite that
of the Patagonian species in miniature, differing chiefly in the pro-
portions of its dimensions, as shown by the subjoined table :—

Macrauchenia Boliviensis. MM. Patachonica. Guanaco. Vieugna,

in. in. in.
Menor. ss 1:45 3:3 1:6 1:3
Greatest width .. 1:2 2:7 ie) 85
Greatest depth .. °85 2-15 95 8

If we take the lengths of the astragali, it will be observed that
their proportions in the Bolivian and Patagonian Macrauchenie are
not the same as those of the cervical vertebra. The astragali bear
the ratio of 1 : 23, while the cervical vertebree gave 1:14. Further-
more, the proportions of length, width, and depth in the two astra-
gali are different. Like the cervical vertebra, the astragalus of WM.
Boliviensis is a, relatively, stouter bone than that of fie Vicugna ;
though instead of being shorter it is a little longer, occupying a
position, in point of absolute length, between the astragalus of the
Vicugna and that of the Guanaco. As the astragalus thus yields
results agreeing very well with those given by the cervical vertebra,
we may safely assume that not only the absolute size, but the pro-
portions of the body of Macrauchenia Boliviensis were nearly those
of the existing Llamas, and differed widely from those of the heavy
and huge Macrauchenia Patachonica.

The tibia.—What remains of the bones of the hind leg confirms
this view of the proportions of Macrauchenia Boliviensis. Ihave the
proximal end of the left tibia, minus the fibula, and with the outer
articular condyle broken away. Below this point, the outer edge
and surface of the fragment are uninjured, and the posterior face is
in good preservation, but the internal face is somewhat crushed.
The muscular ridges on the posterior face are as well marked as in
the skeleton of the Guanaco, and far more distinct than in that of

76 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Nov. 21,

the Vicugna, yielding additional evidence of the adult condition of
the animal, to that afforded by the absence of epiphyses.

The antero-posterior diameter of the tibia, measured from the
posterior edge of the internal articular facet to the anterior edge of
the crest of the tibia, is, in—

M. Boliviensis. M. Patachonica. Guanaco. Vicugna.

in. in. in. in.

2:4 5:4 2:3 2-1,
so that the depths of the proximal ends of the tibiz of the two
Macrauchenie have the ratio of 1 : 27, which corresponds very well
with the proportions of the astragali, and -confirms the conclusions
already arrived at, as to the relative lightness of the limbs of this
species In comparison with those of MW. Patachonica, and as to the
similarity of the proportions of the Bolivian species to those of the
Llamas.

What remains of the outer edge of the tibia is sufficient to prove
that the fibula must have remained unanchylosed to the tibia for a
much greater distance than in the Patagonian species. From the
manner in which the outer tuberosity of the proximal end of the
tibia is broken off, I am inclined to suspect that the fibula was
anchylosed to it at this point ; and perhaps, as in the Auchenia, its
proximal end was represented only by a bony style.

The scapula is represented merely by a mutilated fragment, com-
prising the glenoid cavity and the adjacent parts. The spine of the
scapula is broken off, and the glenoid cavity is somewhat distorted
by the bending of one of its edges; but enough remains to show
that the bone must have agreed with the scapula of Macrauchenia
Patachonica in all essential respects, and that it therefore differed
very widely from that of the Auchenie. In size, however, it nearly
corresponded with the corresponding bone in the latter animal; for
the greatest diameter of the glenoid cavity is 1:2 in., the same
measurement in the Vicugna being 1:0, and in the Guanaco 1:6.

The ulna.—The fragment of the ulna, consisting of part of the
olecranon process and of the sigmoid cavity, is so crushed, that I can
only affirm its general agreement in form with that of Macrauchema
Patachonica, and in size with the same bone in the Llamas.

The lumbar vertebra.—Of bones referable to this region of the body,
again, there is but a single fragment, of value only so far as it con-
firms the conclusions arrived at by the examination of the more
perfect fossils. It corresponds very well with the posterior half of
the centrum of the penultimate lumbar vertebra of MW. Patachonica
in form, and with the corresponding vertebra of Auchenia in size ;
but the crest into which the middle of its under surface is raised,
and which is still sharper than that in the Patagonian species,
diagnosticates it at once from any of the lumbar vertebre of the
Llamas.

The transverse diameter of the articular face is 1-1 in., its vertical
diameter 0-9. The corresponding measurements of the antepen-
ultimate lumbar vertebra of I. Patachonica are 3:0 in, and 2-1; s0

1860. ] HUXLEY—MACRAUCHENIA BOLIVIENSIS. 77

that, as in other bones, the proportions of diverse diameters of the
same bone are not the same in the two species. But as the trans-
verse diameters of the cervical vertebra of the two species are nearly
as 1: 3, and the transverse diameters of the lumbar vertebre are,
also, nearly in the ratio of 1:3, it would seem as if the different
regions of the vertebral column of the two species exhibited the same
proportional correspondence to one another.

The skull.—As no part of the skull of Macrauchenia Patachonica
has yet been discovered (with perhaps the exception of part of the
lower jaw),a great interest attaches to every fragment which promises
to throw light upon this part of its organization ; and I therefore make
no apology for dwelling at some length upon the characters of the
two very imperfect and mutilated portions of the cranium which
turned up among the specimens submitted to me by Mr. Forbes.

The one of these (Plate VI. fig. 3) consists of rather more than half
of the occipital segment of the skull, and exhibits the whole of the
supra-occipital bone, with its strong occipital crest, a part of the
parietal with the sagittal crest, the greater part of the right para-
mastoid process, and the entire right occipital condyle.

As I have already remarked, the sutures are obliterated: and this is
true, not only of those which ordinarily exist between the elements of
the occipital bone in young mammals, but of the lambdoidal suture,
which usually persists for a longer period. The occipital foramen must,
when entire, have had a depressed-oval form, the short, vertical axis
of the oval being about 0°6 of an inch long. The face of the bone
above it inclines upwards and forwards, at an angle of about 50° with
the base of the skull, and presents a sharp ridge in the middle line,
on either side of which the surface of the supra-occipital element slopes
with a shght convexity outwards and forwards, at the sides and below;
while, above, it becomes concave by passing almost vertically upwards
in the middle line, and laterally, bending upwards and backwards
at a right angle with its previous inclination into the occipital crest.

This crest is nearly 0-2 inch thick at the sides, and becomes still
thicker in the middle line, where it joins the sagittal crest. It is
1-1 inch in diameter at its widest part, and about half an inch high.
Its contour is that of a parallelogram, with its angles rounded off,
and the middle of its upper side rather truncated. The lateral
portions project backwards rather more than its centre ; so that, while,
supposing the basi-occipital to be horizontal, a vertical line drawn
through the posterior edge of that bone would nearly coincide with
the contour of its central part, it would pass a little anterior to the
plane of the lateral extremities of the crest. Inferiorly, the thick
lateral portions of the crest divide mto two ridges; the posterior
of which turns slightly inwards and comes to an end, while the
anterior, much sharper at its edge, passes forwards and outwards, and
becomes continuous with the sharp ridge in which the paramastoid
process terminates externally.

Behind this ridge, between the paramastoid process, the occipital
condyle, and the lateral convexity of that part of the occipital bone
which lies above the foramen magnum, there is a deep fossa, which is

78 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Nov. 21,

divided into two portions by a transverse ridge, extending from the
outer and upper part of the condyle to the posterior and inner face
of the paramastoid process. The large precondyloid foramen (pro-
bably somewhat enlarged accidentally) opens into the lower and ante-
rior division of the fossa, beside the condyle, and about 4th of an inch
behind its anterior inferior boundary. The upper boundary of the
foramen magnum is almost straight, and its summit is below the
level of the superior edge of the condyle (when the base of the skull
is horizontal). The condyle is divisible into an upper, smaller, ob-
liquely ascending, and a lower, more nearly horizontal facet. The line
of junction between the two, forming the posterior limit of the con-
dyle, is rounded off and is directed obliquely outwards and upwards.
The moderately convex upper facet looks upwards, backwards, and
but very slightly outwards. It is broad above, where its transverse
diameter amounts to nearly half an inch, and tapers off gradually
to a point below and internally.

The inferior facet, less curved than the other, is 0-6 of an inch
wide behind, hardly more than half that in front, and fully 0-8 of an
inch long. It is slightly convex from side to side, and from behind
forwards, posteriorly, where it looks downwards and outwards ; convex
from side to side, and slightly concave from behind forwards, in front,
where itis directed more horizontally downwards. Its anterior narrow
end has a sharply defined rounded margin, which can be traced to
the anterior boundary of the occipital foramen ; so that the occipital
condyles certainly did not coalesce in the middle line.

The paramastoid process is broken off rather above the level of
the lower boundary of the occipital condyle; but, from the thinness
of the fractured edge, I imagine it did not extend much further. It
is broad and flattened, the direction of its greatest diameter being
from behind and without, inwards and forwards. Its posterior face
is directed as much inwards as backwards, and its outer margin is
sharp, except towards the lower end, where it becomes rounded. In-
ternally, it thickens before rejoining the exoccipital, in front of, and
external to, the precondyloid foramen. The upper part of its anterior
and external face is evidently rough and has united with the mas-
toid, now completely broken away; but it is difficult to say how far
downwards the sutural face extended. The posterior boundary of
the jugular foramen is preserved on the inner side, and in front of, the
thick inner edge of the paramastoid.

The sagittal crest is continued forwards from the triangular pro-
minence common to it and the occipital crest, and at once becomes
very thin and sharp. It is broken off at a very short distance from its
commencement, and at this point it is a quarter of an inch high. Its
superior margin is not parallel with the contour of the middle le
of the parietal region, but has a more marked upward inclination, so
as to lead one to suppose that the crest rose to a considerable height
in the middle of the synciput,—a conclusion which is strengthened
by the great thickness of the parietals (of whose median suture no
trace is visible) in the middle line. The transverse section presented
by the anterior broken edges of these bones is, in fact, triangular,

1860. ] HUXLEY—-MACRAUCHENIA BOLIVIENSIS, 79

and the height of the triangle from its apex, which corresponds with
the base of the crest, to its base (the concave inner wall of the
cranium) is nearly 0-4 of an inch.

In viewing the fragment of the occiput from within, one is sur-
prised by the great thickness of the supra-occipital region, the bone
immediately above the middle of the occipital foramen being half an
inch thick. A well-marked ridge, defining the interior boundary of
the cerebellar fossa, is continued downwards, forwards, and out-
wards, from the anterior boundary of the thick roof of the occipital
foramen. ‘There is no venous canal traceable above the inner aper-
ture of the precondyloid foramen.

If the occiput of Macrauchenia Boliviensis be restored by reversing
the outlines of the right half (as in Pl. VI. fig. 3), thus supplying the
wanting left moiety, the following measurements may be obtained.

Side by side with them I give the corresponding measurements of the
skull of the Vicugna :—

2 : M. Boliviensis. Vicugna.
Transverse diameter of the occiput in. in.
from the outer edge of one para- 1:9 2°25
mastoid to that of the other ....
Ditto from the outer edge of one occi- \ 15 15
pital condyle to that of the other.
The transverse diameter of the occi- 7 7

petal MOrAMEN A... 1s ct eis in.

It will be observed that the two series of dimensions correspond
very closely, the two latter being identical, while the Macrauchenia
appears to have had even a narrower skull than the Vicugna. In
form, the occiput of Macrauchenia agrees better with that of the
Llamas than with that of any other ungulate animal with which I
have compared it.

Thus, in an old Guanaco I find an equally well-marked ridge in
the middle line of the supra-occipital element; the occipital crest is
equally prominent, though not so stout; the sagittal crest is as well
marked, thin and sharp, and, as in Macrauchema, its superior edge
ascends. There is a fossa between the occipital condyle and the
paramastoid, similar in form to that in Macrauchenia, though much
shallower. The occipital condyles are very much alike; and their
relation to the precondyloid foramina is the same in both cases. The
paramastoid has the same proportional breadth; and its greatest dia-
meter is,in both cases, directed from without and behind, inwards and
forwards : in both cases its inner edge is peculiarly thickened. Again,
the paramastoid of the Auchenia, like that of the fossil, is very short,
its apex hardly extending below the level of the occipital condyle.

The occiput of Macrauchenia, on the other hand, differs from that
of Auchema in the much greater thickness of the supra-occipital,
which in the Macrauchenia has fully double the thickness of the same
region in an old Guanaco, whose skull is much larger—in this respect
approaching the Sheep and some other Ruminants, which have this
bone very thick. The supra-occipital, also, is much higher, in pro-
portion to its width, in Macrauchenia than in Auchenia; its lateral

80 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Nov. 21,

contours are parallel, and not divergent outwards and upwards.
There is nothing in the Maer cinnelbonta resembling the deep notch
between the supra-occipital and the base of the paramastoid, into
which a part of the mastoid fits in Auchenia. In contour, in fact,
the occiput of the Macrauchenia resembles that of the Rellaaicrion
more nearly than that of any other Mammal. But, on the whole, I
think it must be admitted that the resemblance of the back of the
skull of the Macrauchenia to that of Auchenia is sufficiently close
to justify the conclusion, that the predominance of the Cameline
type, so marked in the neck, was maintained in the head of the
extinct Mammifer.

The fossil which remains for description (Plate VI. fig. 4) consists
of two fragments of the matrix (a and 6), which fit together, and to
which adhere certain portions of the upper jaw and palate, together
with the fractured remains of three grinding-teeth and part of the
alveolus of a fourth, all of the right side, and in a continuous series.
The alveoli and part of the crowns of these teeth are contained in the
larger fragment of matrix,—the smaller fragment fitting against the
larger and the teeth which it contains, and exhibiting the impressions
of the grinding surfaces of three teeth and of their inner faces, a
portion of dental substance adhering to the latter, in the case of the
two anterior teeth. Of the hindermost tooth nothing is left but the
impression of one fang.

The impression of the grinding surface of the first tooth is nearly
four-tenths of an inch long, convex from before backwards, concave
internally: the outer boundary of the impression is broken away,
a fragment of dental substance adhering to the posterior part of its
inner face. The part of the larger portion of the matrix (a) which
should contain the alveolus of this tooth is absent. The antero-
posterior extent of the coronal impression of the second tooth is a
little more than 0-4 of an inch; it is concave from before backwards
externally, nearly flat internally, and shelves with a slight convexity
upwards and inwards. The inner boundary of the impression is, as in
the preceding case, markedly concave; and a much larger fragment of
tooth-substance adheres to it. The outer boundary of | the impression
is broken away, but much more in front than behind, where its width
is fully 0-4 of an inch. The impressed line which separates this im-
pression from the next is convex forwards. Corresponding with this
impression there are, in the larger fragment of matrix, an almost
entire conical posterior fang, about 0-4 of an inch long, lodged in a
complete bony alveolus, whose outer wall is broken away, and the
posterior half of a similar alveolus for an anterior fang: there is no
trace of a third alveolus or fang; and, indeed, there seems to be no
room for one. The fang which exists is connected below with a
portion of the crown; but this is so broken, that all that can be
remarked of it is its marked internal convexity.

The coronal impression of the third tooth is half an inch long;
like the preceding, its face shelves upwards and inwards. The poste-
rior part of its outer mar gin is broken away; butit is clear that this
crown was quite as wide as that which preceded it, if not wider ;

1860. ] HUXLEY—MACRAUCHENIA BOLIVIENSIS. 81

the surface appears, however, to have been more evenly flat. The
inner perpendicular face of the impression presents two concavities,
separated by a slight ridge.

More of this tooth is preserved than of any other; the outer wall
of the maxilla is, for the most part, preserved over it, and encloses the
alveoli of two external fangs. There is evidently at least one, and
perhaps two, internal fangs. The whole thickness of the inner and
posterior part of the crown is preserved, and the posterior and inner
half of its worn face; the rest of the tooth is broken away. The
posterior and outer fang, partially exposed, is 0-3 of an inch long,
conical, and slightly inclined backwards, as well as upwards and
inwards. The crown, where it joins the fang, is 0-4 of an inch long;
so that it must have widened a little below. The vertical height of
the crown of the tooth posteriorly and internally is hardly more than
0-15; anteriorly and internally it is broken ; but, when entire, it had
a height of at least 0-2. The inner surface of the tooth is divided into
two tolerably well-marked subcylindrical faces, which correspond with
the impressions on the inner wall of the coronal impressions.

The outer moiety of the crown is altogether broken away ; the inner
moiety, broken anteriorly, exhibits in its posterior half a smoothly worn
facet, concave from before backwards, and inclined not only down-
wards but slightly backwards. A narrow fringe of enamel appears to
surround the worn dentine of this face, which is wider in the middle
than at the two ends. The true outer face of the enamel can be
traced from the inner face of the tooth, continuously, round the pos-
terior boundary of this worn facet, and as far as its most dilated.
portion on the inner side. It is concave outwards, and presents a
slight inflexion midway between the posterior end of the facet and
its middle dilatation. Beyond the dilated middle of the facet, its
enamel-wall seems to have been united with that of the opposite
half of the tooth; but it is traceable forwards, becoming concave
externally, past the anterior end of the worn facet, to the anterior
margin of the tooth, where it bends round and again becomes con-
tinuous with the enamel of the inner face.

This tooth, therefore, appears to have possessed an internal divi-
sion, elongated from before backwards, surrounded by a narrow band
of enamel,—having its inner contour produced into two convexities,
separated by a slight vertical depression, while its outer wall pre-
sents two concayities, separated by a slight ridge which lies rather
behind the level of the depression on the inner face. By use, the
posterior part of this division wore down into a facet, concave from
before backwards, and separated, by a transverse ridge, from the facet
in front of it. A longitudinal fossa separated the posterior moiety, at
least, of this division of the tooth from the outer division.

Imperfect as is this fragmentary grinder, certain important con-
clusions may, I conceive, be very safely drawn from its structure.
The predominance of the longitudinal, to the exclusion of transverse
valleys and ridges in the crown of the tooth, the distinct, though
not strongly marked, crescentic form of the internal division of the
tooth, and its short crown, remove it from the teeth of any known

VOL, XVII,—PART I. 6

82 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Nov. 21,

Perissodactyle Mammal, and lead one, at once, to seek its analogue
among the Artiodactyla; and of these the Ruminants alone, so far
as I know, offer anything like it. The inner grinding-surface of
any true molar of a Ruminant, however, exhibits two ridges and
three depressions; while that of the Macrauchenia has only one ridge,
with a concave shelving depression behind, and doubtless, in the
perfect condition, another in front; in other words, it has the eon-
tour exhibited by one of the hinder premolars of a Ruminant. The
inner division of a posterior premolar of Auchenia has its convex
inner surface undivided by any vertical depression; and its outer,
posterior margin exhibits no marked inflexion: but such an inflexion
exists in the corresponding teeth of the Giraffe and of many Deer,
in some of which latter a vertical groove, dividing the inner face
into two convexities, may also be noted.

I am of opinion, therefore, that the tooth in question 1s a poste-
rior premolar, and that it was constructed upon the Ruminant type..
In this case, however, the dentition of Macrauchenia must have
departed widely from that of the Camelide ; for there were certainly
two teeth with flat grmding crowns in front of that just described,
which would give, at least, three premolars in all, or as many as are
found in ordinary Ruminants.

I am strengthened in the conviction that there were as many as
three premolars, by the rest of the structure of this interesting frag-
ment. Within the series of teeth just described, in fact, it presents
a considerable portion of the roof of the palate, some of whose bony
matter remains. At a distance of half an inch from the inner wall
of the posterior premolar, a longitudinal sutural line traverses the
whole length of the palatine surface, and ends abruptly (in conse-
quence of the fracture of the matrix) as well behind as in front.
Its posterior end is 1-2 of an inch behind a transverse line drawn at
the level of the posterior margin of the last premolar. Opposite and
behind this tooth, the right half of the palate is marked by what
might hastily be taken fora suture, but which is nothing but a frac-
ture. Behind it, and 0-9 of an inch in front of the posterior end of the
longitudinal suture, two curved transverse lines, convex forwards,
which I believe to be the maxillo-palatine sutures, pass into the
longitudinal suture.

Thus, it is clear that the palate must have extended back for 1:2
of an inch behind the third grinding-tooth.

Supposing this tooth to have been succeeded by three others whose
length, if they were molars, would be probably between 0-6 and
0-7 of an inch, it follows that the posterior margin of the palate
must have extended, at least, as far back as the posterior margin of
the second molar. This is further than it extends in the Auchenie
(the very forward extension of whose palatine aperture is excep-
tional among the Artiodactyla), but it is not so far as in the Camel,
where the posterior boundary of the palate is opposite the middle of
the last molar*.

* The attempt to differentiate the Artiodactyla and Perissodactyla absolutely
by the position of the posterior margin of the bony palate is fallacious. On an

1860. | HUXLEY—MACRAUCHENIA BOLIVIENSIS. 83

This backward extension of the palate is, so far as it goes, in
favour of the view to which the consideration of the dentition and
the structure of the occiput leads, viz. that the cranium of the
Macrauchenia was constructed upon an essentially Artiodactyle type.

The following are the dimensions of the palate and teeth of Ma-
crauchenia Boliviensis, and those of the corresponding parts in the
Vicugna :—

Macrauchenia. Vicugna.

; Let eee
eee \ about 1:0 1-25 (at widest).
Antero-posterior length f more than 2:0] 2.9

of four grinders.... [less than 2:5 f Ea

The narrower palate of the Macrauchenia agrees with its narrower
occiput, while it exhibits the same general correspondence with the
Vicugna as has been met with in the hmbs and vertebre.

Thus I conceive that an attentive examination of these scanty
remains is sufficient to prove that, when they were imbedded, there
lived in the highlands of Bolivia a species of Macrauchenia not half
as large as the Patagonian form, and having proportions nearly as
slender as those of the Vicugna, with even a lighter head; and it is
very interesting to observe that, during that probably post-pleistocene
epoch, a small and a large species of more or less Auchenoid
Mammal ranged the mountains and the plains of South America
respectively, just as at present the small Vicugna is found in the
highlands, and the large Guanaco in the plains of the same con-
tinentt.

The structure and geological date of the genus Macrauchema may
serve, if taken together, to point an important paleontological moral.
Professor Owen, in the able memoir cited above, has clearly ‘pointed
out the remarkable combination of Artiodactyle and Perissodactyle
characters exhibited by Macrauchenia, which unites the eminently
characteristic cervical vertebre of the Artiodactyle Camelide with
the three-toed fore foot and the triply trochantered femur of the

average it is doubtless true that the bony palate extends further back in the former
than im the latter; but the bony palate extends to a line joining the anterior
edges of the last molars in Hyrax; while in the full-grown Guanaco, a similar
line is 0-4 of an inch behind the posterior boundary of the palate.

* The six grinding-teeth of the lower jaw, which Professor Owen has provi-
sionally referred to Macrauchenia (British Association Reports, 1846), are said
to form a series 9 inches long. A series of six such teeth of the lower jaw
of Macrauchenia Boliviensis could not have exceeded 4 inches in length, and
was probably shorter. Under these circumstances, the heads (as measured by the
teeth) of the two species would be in nearly the same proportion as their
astragali, and in very different proportions from their cervical vertebre. ‘This is
not improbable ; for the Vicugna has a much lighter head than the Guanaco, if the
cervical vertebrae be taken as the standard. The length of the fourth cervical of
the Vicugna is to that of the same bone in the Guanaco as 1:14, while the length
of the head in the two is as 1: 12.

+ As the Guanaco ranges into the highlands, it may not be a too sanguine
expectation to hope for the future discovery of remains of the great Macrauchenia,
also, in Bolivia.

G 2

=

84 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Noy. 21,

Perissodactyla ; and with an astragalus which, in the apparent entire
absence of any facet for the cuboid, is, I may affirm, more Perisso-
dactyle than that of any member of the order, except Hyrax.

None of the older Tertiary mammalia can produce such strong.
claims to be considered an example of what has been termed “a
generalized type” as Macrauchenia ; and yet there seems little doubt
that the latter is the South American equivalent, in point of age, of
our Irish Elk!

Again, Macrauchenia, alone, affords a sufficient refutation of the
doctrine, that an extinct animal can be safely and certainly restored
if we know a single important bone or tooth. If, up to this time,
the cervical vertebree of Macrauchenia only had been known, palecn-
tologists would have been justified by all the canons of comparative
anatomy in concluding that the rest of its organization was Came-
lidan. With our present knowledge (leaving Macrauchenia aside), a
cervical vertebra with elongated centrum, flattened articular -ends,
an internal vertebral canal, and imperforate transverse processes, as
definitely characterizes one of the Camel tribe as the marsupial bones
do a Marsupial,—and, indeed, better; for we know of recent non-mar-
supial animals with marsupial bones. Had, therefore, a block eontain-
ing an entire skeleton of Macrauchenia, but showing only these por-
tions of one of the cervical vertebre, been placed before an anatomist,
he would have been as fully justified in predicting cannon-bones,
bi-trochanterian femora, and astragali with two, subequal, scapho-
cuboidal facets, as Cuvier was in reasoning from the inflected angle
of the jaw to the marsupial bones of his famous Opossum. But, for
all that, our hypothetical anatomist would have been wrong; and,
instead of finding what he sought, he would have learned a lesson
of caution, of great service to his future progress.

EXPLANATION OF PLATE VI.

Fig. 1. Cervical vertebra of Macrauchenia Boliviensis, Huxley; restored from
the opposite side, posteriorly. ;
1 a. The same vertebra, viewed from in front.
1 6. The same vertebra, viewed from behind.
2. Astragalus (left), from above.
a. - » trom below.
b. 5 ,, from the outer side.
3. Fragment of the occipital portion of the cranium, restored in outline.
3 a. The same fragment, viewed from without and laterally.
4. Part of the upper jaw and palate, and lateral view (@) of the crown of the
most perfect tooth. ;
4a. Side-view of the large fragment of the matrix containing the teeth, with
the smaller fragment, exhibiting the coronal impressions, adapted to it.

€

bo bo b

PLVL

is

XV]

Yol

Quart. Journ Geol. Soc

G West del % ith.

MACRAUCHENIA BOLIVIENSIS.

1860. | NICOL—N.W. HIGHLANDS. 85

DercemBer 5, 1860.

William Salmon, Esq., Ulverstone, Lancashire; Peter Higson,
Esq., One of H. M. Inspectors of Coal-mines, Broughton, near Man-
chester ; John Spencer, Esq., Bowood, Wilts; Alexander R. Binnie,
Esq., C-E., 7 Upper Lansdowne Terrace ; George James Eustace,
Esq., Arundel House, Clifton Road, Brighton; F. D. P. Dukinfield
Astley, Esq., Dukinfield, Cheshire, Arisaig, W. B., and 67 Eaton
Square; and Thomas Baxter, Esq., 1 Castle Place, Worcester, were
elected Fellows.

The following communication was read :—

On the Srructure of the Norra-Wesrern Hicunanps, and the
Rerations of the Gueiss, Rep Sanpstone, and Quarrzire of
SurHERLAND and Ross-suire. By Jamus Nicot, F.G.8., F.R.S.E.,
Professor of Natural History in the University of Aberdeen.

Contents.

Introduction, and object of paper. | Loch Broom.
Durine Limestone. | Loch Maree and Gairloch.
Loch Erriboll Sections. Loch Torridon and Loch Carron.
Overlying Red Sandstone and Quartzite South of Skye.

at Tongue. General considerations.
Loch More Sections. Distribution of the Rocks.
Lochs Glen Coul and Glen Dhu. Nature of Formations.
Section of Glasyen. Strike of the Beds.
Structure of Assynt and Ben More. Mineral character of the Rocks.
Loch Ailsh Section. | Conclusion.

Elphin and Craig-a-Chnockan.

Introduction.—In a paper read to the Society in 1856, and pub-
lished in vol. xi. p. 17-39 of the Geological Journal, I pointed out
some of the features of the Gneiss, Red Sandstones, and Quartzites
which form such prominent objects in the geology of the north-west
of Scotland. ‘I then proved (contrary to the opinion previously en-
tertained) that the Red Sandstone of the North-west Highlands, and
especially that of Loch Broom and Applecross, was wholly inferior
to the quartzite, which rests on it in an unconformable manner, and
spreads out wider to the east. In the same paper I showed that the
Assynt and Durness limestone forms the upper member of this series,
and that the supposed higher quartzite of Ben More is only the same
quartzite rising from under the limestone. In regard to the rela-
tion of the quartzite to the eastern gneiss, I stated that, though
some of the sections appeared to confirm Dr. Macculloch’s view that
there are in Sutherland two formations of gneiss—an older below
the quartzite, and a newer superior to it,—still the presence of
intrusive rocks and other marks of disturbance in the sections I had
examined rendered this conclusion less certain and satisfactory than
might be wished. In order to determine this most important ques-
tion, affecting the entire geological history and structure of the
north of Scotland, I have subsequently visited this region four times,

86 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 5,

and examined all the principal sections and almost the entire tract
of country from the north coast of Sutherland, to Loch Alsh and
Skye in the south, and from Caithness on the east to the Lewis on
the west. I now propose to lay the results of these investigations
before the Society, as confirming or correcting the views given In my
former paper. ‘This is the more necessary, as, whilst some of my
statements have been controverted, other statements may seem to
support conclusions which I now feel assured are erroneous. The
wide region over which these observations extend, and the great
importance of the questions involved, together with the weight of
authority opposed to the views I support, must form my excuse for
the length of this paper and the full details given of some sections.
Object of this paper.—As it may render the bearing of the special
sections noticed more evident, I may state that there is no difference
of opinion in regard to the first part of the series of formations as
established in my paper of 1856. All observers now admit that there
is only one great formation of Red Sandstone on the north-west coast,
resting unconformably on gneiss, and covered, in many cases also un-
conforr mably, by « juartzite, and this by the fossiliferous lmestone of
Durness. But the further order is matter of discussion. I regard
this limestone, in Durness, Assynt, Loch Broom, and Loch Keeshorn,
as the highest member of the older formations in this region (fig. 1).

Vig. 1.—Diagram-section of Sutherland and Ross.

d. Limestone. c?. Fucoid-beds. c!, Quartzite. b. Red Sandstone.
a. Crystalline schists. z. Granulite or syenite. J. Fault.

On the other hand, it has been affirmed* that it is overlain by an
upper quartz-rock and limestone, and that these are in turn “ clearly
and conformably covered,” or “followed symmetrically upwards, by
mica-schists, flagstones, and a younger gneiss.” This paper is
designed to prove that no such clear, conformable, or symmetrical
upward succession is to be found, but that the line of junction,
where this conformable succession is said to occur, is clearly a line
of fault, everywhere indicated by proofs of fracture, contortion of the
strata, and powerful igneous actiony.

Durine Iimestone.—Beginning our sections in the north, the first is -
that of the Durine limestone. The section given in my former paper ?,
though showing the true general relations of the beds, must be eor-

* Sir R. I. Murchison, ‘Siluria’ (3rd edition), p. 553. See also Murchison
‘““On the Succession of the Older Rocks in the Neetu eee Counties of Scot-

land,” Quart. Journ. Geol. Soc. vol. xv. p. 352, and ‘‘ Supplemental Observations,”
éb. vol. xvi. p. 215, &e.

t The diagram fig. 1, compared with the similar section fig. 2 in p. 217

of vol. xvi. of. Quart. Journ. Geol. Soc., will bring out this difference of views
more clearly.

{ Quart. Journ. Geol. Soc. vol. xiii. p. 23. fig. 5.

Fig. 2.-—Section of the Durine District,

-an-na-binn.

4
So
‘e)
AF) in
<=] ©
os
: q
e —
fas) =
S >
ie}
te °
Ss no
3 —
m i.
ES
co)
>
as]
O
fo}
je)
§ ;
w 2
I
oe
o
: iF
= g
in) om
5 ss
ee 0)
3 |
vA S
[=
= B
m ore
oe Fs
5 Ss
= ids)
S
S
as
2 .
iB 8
2 s
tea mn
g t
eS <
= =
aS =
° .
S
ig
>
&
o
3

ce’. Quartzite.

d. Limestone.

Fav-out Head.

fy.

NICOL—-N.W. HIGHLANDS. 87

rected as to details by that now given*
(fig. 2). Beginning at the western extre-
mity, the magnificent promontory of Far-out
Head, 315 feet high, consists trom top to
bottom of fine-grained white or light-
coloured mica-slate, in thin even beds. The
dip is from 20° to 25°, or rarely 35°, to EK.
35° 8. at the Head; but near Old Castle
Point, where the rock is also darker in co-
lour, always to the north of east (H. 25°-35°
N.). From the regular dip of the beds, the
thickness of this mass of mica-slate must. be
above 2000 feet if the section is unbroken,
and not less than 1000 feet if a fault occurs
between Far-out Head and Old Castle Point.
In mineral character it is quite identical
with the mica-slate on the east of the quartz-
ite at Erriboll, and with the mica-slate of
Melness on the Kyle of Tongue. It has on
this account been said to overlie the Durince
limestone ; but, after repeated careful exami-
nation of the sections, which are most clearly
exhibited on the coast, I have been unable to
detect the smallest trace of limestone below
the mica-slate, or of mica-slate above the
limestone. It seems impossible to believe
that a mass of mica-slate, at least 1000 feet
thick, could have been so thoroughly swept
away from the surface of the limestone-field
for many miles in extent, had it ever existed
above it.

Near Balnakeil and Sangoe Bay the mica-
slate appears to dip under the lmestone ;
but, as shown in the section, it is cut off from
it by a fault. This limestone forms a great
contorted mass, 128 feet high, and is in many
parts a red-coloured breccia; but it dips on
the whole to the S.E. The brecciated struc-
ture is due to a mass of hornblende-rock or
serpentine which rises up in Sangoe Bay,
bringing with it portions of altered quartzite
and mica-slate. The igneous and metamor-
phie rocks extend south to Loch Calladale,
and have evidently been forced up through

* The sections in the following paper run generally
from west to east, and, for more ready comparison,
are all drawn as seen from the south. The directions
in this paper are also true, having been corrected
for the magnetic variation, which in Sutherland is
about 29° W.

88 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

the limestone, which is broken and contorted near them. The lime-
stone again forms the coast, intersected, however, by another N. and
S. line of fault at the Smoo Cave. Near Sangoe Beg the quartzite
appears, forming a small wedge-shaped fragment, and is represented
by Mr. Cunningham, who first figured the section, as dipping con-
formably under the limestone*. This is no doubt its normal posi-
tion ; but in this place the rocks are separated by a fault and crush,
which has broken up the quartzite into an incoherent breccia.
Beyond Cnoc Garrow the quartzite is succeeded by the ridge of gneiss
dividing the vale of the Dionard from Loch Erriboll. The ridge runs
S.8.W., but the strike of the beds is nearer N.W. (N. 48° W.), and
the dip at 70° to 85°, toS.W. or N.E. It is everywhere penetrated
by veins and masses of red granite and hornblende-rock, and has
evidently been tilted up on the west side since the deposition of the
quartzite, which rests in a thin and often-interrupted layer on its
eastern side, sloping down to Loch Erribollt. Small fragments of
quartzite also occur on its seaward extremity.

This section of the Durine district is important, as proving that
the limestone is the highest formation in the series, and is nowhere
covered by higher quartzite or mica-slate ; these rocks, where found
in the centre of the section, being evidently brought up from below,
and thus underlying, not overlying, the limestone. It also shows
that the whole district 1s broken up by faults running from N.N.E.
to S.8.W., and that the masses of strata have generally been tilted
up on the west.

Sections on Loch Erriboll—tThese facts serve to explain the more
complex sections on the east side of Loch Erriboll. The first of these
(fig.3) runs from near Camas-an-duin, in an east-by-south direction,

Fig. 3.—Section of Camas-an-duin, Loch Erriboll,

W.

a!
.

Marshy valley
and Fault

BS
WAS
Sow

Si

d. Limestone. c?. Fucoid-beds. c!. Quartzite.
a. Mica- and tale-slates. s. Granulite, with fragments of slate.

across the ridge to Loch Hope. On the shore south of Camas Bay,
the strata are seen in their regular normal order: first the quartzite
(c') in curved beds, but dipping on the whole to W.; then (c*) the
fucoid-beds, and above all the limestone (d),in broken irregular strata,
but also with a westerly dip. The limestone forms a low hill, sepa-

* Cunningham, Geognostical Account of Sutherland in Prize Essays of the
Highland Society, vol. xi. (1839) p. 97, and plate 7. fig. 4. This quartzite
does not appear in my former section, which runs further south than it extends.

+ Far too great thickness is assigned to this part of the quartzite in my old
section, Quart. Journ. Geol. Soe. yol. xiii. p. 23. fig. 4c.

1860. | NICOL—-N.W. HIGHLANDS. 89

rated from the main ridge by a low marshy valley, indicating a line of
fault. This fault is also proved by the quartzite, with its characteristic
annelid-tubes (Pipe-rock), dipping first 78°, to KE. 30° 8., and then 70°,
to W. 10° N. On the main ridge the same quartzite forms a great
curved face of rock, dipping at 50°-65°, to W. 33° N., and higher
up 74°, to W. 25°N. The top of the ridge consists of a granitoid
igneous rock or granulite*,in part overlain by quartzite. This
mass or vein varies from a few yards to above a fourth of a mile in
width. Beyond it, on the east side of the ridge, mica- and talc-slates
occur in thin regular beds, and often identical in character with the
rocks of Far-out Head. The prevailing dip is 15° to 25°, to 8. 30° E.,
but varies considerably near the granulite, where the beds become
contorted and interlaced with igneous matter. In a deep valley to
the north, a more complete section of the interior of the hill is seen ;
the granulite widening out to half a mile or more, throwing off the
strata on each side, and involving large fragments of the mica-slate,
with the laminz turned in various directions. As these fragments
of mica-slate are found in the mass of the igneous rock where it
rises up below the quartzite, and, of necessity, have been derived
from a still deeper formation, they prove indisputably that the mica-
slate is the lower and older rock, and therefore cannot normally
overlie the quartzite.

Further north, the igneous rock widens out greatly in Arnaboll
Hill, and has produced some remarkable changes on the strata.
Thus, on Camas Bay, in the continuation of the fault in the former
section, the quartzite dips at 53°, to 8. 64° E., and apparently
below the igneous mass of the hill. But the openings of the
annelid-tubes, and the ripple-marks, which are regularly found on
the upper surface of the beds, are here on the lower faces, showing
that there has been a complete reversal of the strata. Still proceed-

Fig. 4.—Section of Drium-an-tenigh, Loch Erriboll.
W. Heilam Inn. Loch Hope. E.

d. Limestone. c?. Fucoid-beds. c!, Quartzite.
x. Granulite (termed “ gneiss” by Mr. Cunningham).

ing northwards we come to the remarkable section of Drium-an-
tenigh (fig. 4), described and figured by Mr. Cunningham as an

* It is difficult to assign a name to this rock. In general it is a mixture of
compact felspar and quartz, often with an imperfect laminar texture. With
these, hornblende or tale or scales of bronzite become occasionally intermixed.
But in other places it passes into a distinct crystalline binary granite of ortho-
clase and quartz, or into felspar-porphyry or diorite, and where in contact with
limestone into a kind of serpentine. With all this diversity it exhibits a com-
munity of character, more easily recognized than described, along the whole line
from Whiten Head to the Sound of Sleat. I have often used the term granulite,
as the most generally applicable.

90 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 5,

example of gneiss conformably overlying the limestone and quartzite.
It might be sufficient to state that the rock which he describes as
gneiss is the intrusive granulite-rock of the last section*; but, as
illustrating the structure of the country, some further details are
necessary.

At Heilam Inn, on Loch Erriboll (fig. 4), the limestone dipping
10°—20°, to 8. or 8.E., but in broken flexured beds, forms both the
peninsula and the hill on the mainland to about the line of the road.
The next ridge consists of the quartzite, dipping on the west side at
65°, to W. 10° N., and on the east of the ridge 44°, to W. 5° S.
Crossing a small valley, the quartzite is again seen, dipping 83°,
W.10°N., and further on the fucoid-beds, dipping 64°, to S. 45° E.
The rocks are hidden for about 100 yards by grass and detritus ;
but at the foot of the cliff the same beds crop out, dipping in one
place at 20°, to E. 35° 8., and in another at 6°, toS. 10° W. As
already stated, these beds are covered, not by gneiss, as in Mr.
Cunningham’s figure, but by the granulite or eruptive rock form-
ing the great mass of the hill. It has clearly broken through the
strata, resting in one place on the fucoid-beds, in another on the
quartzite, and further east, towards Loch Hope, is overlain by
quartzose beds dipping 25°, to E. 30° 8

The relations of the rocks i in this section are quite clear and con-
sistent. No overlying gneiss is seen in it, and the mica-slate
is separated from the quartzite by the whole igneous mass of Ben
Arnaboll. The quartzite is, however, thrown east as far as Loch
Hope ; and the junction is then formed partly by the lake, partly by
the River Hope to its mouth. In the hills north-east of Hope
Ferry there is another outburst of igneous rock, here felspar-
porphyry; and at Whiten Head it again appears in great force
in the line of junction, intruding partly on the quartzite, but
chiefly on the old slates to the east. In this trackless region the
sections are best seen in sailing along the coast; but one single
fact is decisive of the true relation of the mica-slate and quartzite
series. North of Loch Hope Ferry the fucoid-beds and limestone
entirely disappear, and only the lower part of the series, or the
quartzite, comes in contact with the eastern gneiss or mica-slate.
This is the necessary result of the beds along the line of fault
having been more exposed to denudation in the north, during the
gradual elevation of the land, from the wide and stormy northern
ocean, but is quite inexplicable on the hypothesis of conformable
upward succession. It has indeed been asserted that this is not
the quartzite below the limestone, but another quartzite above it.
That this is not the case is, however, proved by the quartzite near

* See Cunningham, Geog. of Sutherland, p. 99, and plate 8. fig. 2. Though
a very acute observer and well acquainted with rocks, Mr. Cunningham has
in this and some other instances been misled by the strong Wernerian views on
the origin of certain rocks which he entertained. In consequence of this bias he
entirely mistook the nature of these igneous rocks, which were e altogether over-
looked until I drew attention to them in the summer of 1859. This is also true
of the similar rock on Loch More. Compare Note, p. 94.

1860. | NICOL—-N.W. HIGHLANDS. 91

Loch Cragey passing below the limestone of Heilam Hill; by the
same quartzite again rising up from below the limestone on the
coast near Tor-a-vu; and by the fucoid-beds and limestone over-
lying it in regular order in several places south of the road to Loch
Hope Ferry. The occurrence of an upper quartzite in this place is
thus not merely without proof, but contrary to many clear sections,
and, we shall soon find, has no support in any other locality*.

The junction of the quartzite and mica-slate in the hills south of
our first section towards the head of Loch Erriboll equally proves
that the mica-slate is the lower formation. In this place the
igneous rock has generally thinned out, or rather, instead of being
concentrated in a single mass or vein, becomes intermixed with the
lower mica- and talc-slates in innumerable fine threads or lines.
So intimate is this mixture, that, in many places, it is difficult
to say whether the rock should be classed as igneous or stratified.
Occasionally, however, larger masses occur, as near the road from
Erriboll to Ault-na-harrow, where it forms a boss 50 to 100 yards in
diameter, and in the picturesque rock of Craig-na-feolin, Whether
concentrated in mass or dispersed in threads, the igneous matter is
far more abundant in the lower schists than in the quartzite, the
thick hard beds of the latter having apparently resisted its upward
progress and thus caused it to spread out in the inferior formation.
This distribution, therefore, of the igneous rock is another proof
that the eastern mica-slates are the lower formation, as, on the
supposition that the quartzite was the lower formation, it ought to
have been more powerfully invaded by the igneous rocks than the
schists resting upon it T.

This intrusion of igneous matter, swelling out and expanding the
lower schists along the line of fault, has produced some complexity
in the sections. In many places the quartzites and mica-slate dip
approximately in the same direction, but are separated by a fault,
frequently marked by a low marshy hollow. A more interesting
section is seen in a small stream above Erriboll House (fig. 5). The
upper part of the ridge consists of talcose mica-slates (a) interlaced
with lines of red felspar. The dip near the top is 50°-60°, to HE.

* This hypothesis of an upper quartzite requires not merely the repetition of
the so-called “lower” quartzite with its characteristic annelid-tubes and peculiar
mineral characters, but also of a second group of fucoid-beds and a second lime-
stone, identical in order and character with those below! But if such upper
beds exist, they ought then to have appeared in the Whiten Head sections, and
their absence is thus fatal to the notion of “conformable upward succession ”’
in this region.

t* These strata (chloritic, taleose, and micaceous schists), whatever may be their
mineral character, are riddled by the intrusive rock, and in parts much hardened
and altered.” —Murchison, North Highlands, Quart. Geol. Journ. vol. xvi. p. 285.
In p. 253 Sir R. I. Murchison describes them as “interwoven with the meta-
morphic Lower Silurian strata,” ¢.¢. with the eastern gneiss; and also affirms
that *‘the granitic felstones and syenites so largely developed in the eastern parts
of Assynt . .. . rarely, if ever, occur between the limestones and the upper
quartz, but chiefly either in the latter or in the younger or overlying flagstones ”
(p. 253). That is, according to my view, the igneous rocks are most abundant
in the crystalline schists below, and in the quartzite where in contact with them.

92 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 5,

30° N., but below decreases to 15° or 20°, and the beds are broken
and irregular. Lower down, the burn tumbles over a thick mass of

Fig. 5.—Section near Erriboll House.

d. Limestone. c?, Fucoid-beds.
c*™ Quartzite. cl. Quartzite.

a. Mica- and tale-slate, with granitoid veins.
quartzite, very indistinctly stratified, but apparently dipping at 66°,
to 8. 10° E., and resting on the red fucoid-beds (c°) dipping at 50°,
to E. 20°-30° N. Below them is a bed of hard reddish quartzite
(c*) dipping 35°, to E. 20° S8.; and further down the common dark
bluish-grey limestone, much fissured and contorted, but with a dip
of about 68°, to E. 30° S. The limestone appears to form all the
under part of the hill and the low ground to the loch. In this
place the quartzite appears to rest on the limestone and dip below
the mica-slate, but the succession of the groups shows clearly that
this is the result of an upheaval and inversion of the strata. The
regular order in the whole north-west of Scotland, from Durness to
Loch Keeshorn, is quartzite (c'), fucoid-beds (c*), and limestone (d) ;
and we must either admit this inversion, or make the improbable
assumption that the succession of the deposits has been completely
reversed in the space of a few hundred yards, and only in this very
limited zone along the declivity of this ridge.

The same relation of the beds is seen near the Ault-na-harrow
road, though, from the more powerful intrusion of the igneous rock,
the strata are more irregular in dip and more highly contorted near
the line of junction. The quartzite is so compact as to resemble
calcedony, and shows no marks of bedding. The fucoid-beds and
limestone are in some places nearly vertical, in others more horizon-
tal. The fine-grained talcose mica-slates also, which near* the
quartzite and intrusive rock dip at 35° and 30°, to E. 60°S., further
east dip at 10° or 5°, to E. or E. 15° 8S. Over the hill, towards
Loch Hope, the dip becomes even lower, so that the undulations of
the strata cause them in many places to dip to the west.

Overlying Red Sandstone and Quartzite of Tongue.— Another
proof of the true succession of the formations in the north of
Sutherland appears in the vicinity of Tongue, about eight or ten

1860. ] NICOL—N.W. HIGHLANDS. 93

miles to the east of the sections just described. On the east side
of the Kyle of Tongue several remarkable masses of red conglo-
merate rest on the gneiss. These have hitherto been allowed to
remain in the Old Red or Devonian formation, though separated
from the nearest undoubted Old Red strata, on the east of Strathie,
by an interval of eighteen miles. This summer (1860) I examined
these conglomerates, in the expectation that they might throw some
light on the history of this western region. They consist of rounded
or angular fragments of coarse- or fine-grained gneiss, mica-slate,
granite, felspar-porphyry, and vein-quartz; but I could find no trace
of the red sandstone, quartzite, or limestone, which now form the
great ranges of mountains in the west. This entire absence of any
fragments of these rocks, which have formerly covered to the depth
of some thousand feet a tract of country forty or fifty miles wide
and more than a hundred miles long, and not ten miles distant,
seems‘ altogether inexplicable on the supposition that the two
deposits are of widely different age—the one Cambrian and Lower
Silurian, the other Old Red or Devonian. The conclusion seems
therefore irresistible that these Tongue conglomerates are identical
in age, as they are in mineral character and composition, with the
red conglomerates and sandstones of the west coast. This identity
is confirmed by the occurrence of the overlying quartzite on Cnoc
Craggie, near Loch Laoghal. The greater part of the hill consists
of the conglomerate overlain on the south side by the quartzite in
thick irregular beds. The preservation of these interesting frag-
ments seems due to the great syenite-eruption of Ben Laoghal,
which has at once hardened the beds and preserved them from
removal by denudation. In this place, therefore, there is clear evi-
dence that so far from underlying all the gneiss of central Suther-
land, the red sandstone and quartzite of the west are again found
resting upon it ten miles to the east of the supposed overlap.

Loch More Section.—The next point to the south where the quartz-
ite is said to be overlain conformably by gneiss is near the north-west
end of Loch More. In Mr. Cunningham’s section this relation of the
rocks is very distinct; but on the ground the phenomena are quite
opposed to this view, as shown by the section fig. 6, the result of a

Fig. 6.—Section on the South Side of Loch More.

We Ben Stack. Craig Dhu. Ben Leick. ut

IY

e. Quartzite. aa. Gneiss with granite veins. a. Gneiss.
x. Granulite (termed “ gneiss”’ by Mr. Cunningham).

careful examination of the locality in two separate seasons. At the
western extremity of Loch More, the quartzite (c’) rests in a long

94 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

bold cliff on the gneiss (a), which forms Ben Stack and the moun-
tainous region to the west coast. Beyond the Lodge, granulite like
that on Loch Erriboll breaks up through the quartzite, and may be
traced for more than a mile along the upper part of the mountain,
where it is free from the detritus that covers the slopes near the
road and loch. Mr. Cunningham represents this rock as gneiss* ;
but it is truly unstratified, and its intrusive character is shown by
the quartzite having been pushed up and resting on it in broken
and nearly vertical beds, dipping 85°, to N. 40° W. Higher up the
lake this igneous rock meets the gneiss of Ben Leick, exposed in
lofty vertical cliffs, and dipping first 20°, to E. 75° N., and then
15°, to E. 80° N. On the south side of the ridge, towards Strath-
na-carrian, the gneiss, full of igneous veins and greatly contorted,
has quite the aspect of the gneiss round Loch Inver and Scourie, but
dips at 40°, to E. 20° $8. It seems merely the continuation of the
beds seen in the west part of the section, in Ben Stack. That there
is in this place no conformable upward succession from quartzite to
gneiss is proved not merely by the clear break in the section, but
even more by the quartzite, which, on the north side of Loch Stack
and Loch More, has a thickness of 800 to 1000 feet, as well seen in
the front of Arkle and Foinaven,—on the south side of these lakes
disappearing, except a few fragments not the tenth part of that
thickness. his is the necessary result of denudation over a line of
fault ; whereas no amount of denudation could ever show less than
the full thickness of the deposits in any section of conformable
strata. As shown in the figure, I have been unable to detect any
trace of quartzite or limestone on the east side of the imtrusive
rock.

Lochs Glen Coul and Glen Dhu, and Glasven.—The quartzite,
with the same degraded dimensions, ranges across to Lochs Glen
Dhu and Glen Coult, and in the rugged mountains that surround
the inner recesses of these noble sea-lochs is said to be again over-
lain by gneiss. This, however, is a mere optical deception, caused
by the rocks being seen from the low ground or the sea; as the
quartzite, though “dipping eastwards, only abuts on the rounded
knolls that rise up behind, and is generally separated from them by
a low marshy valley. The rock too, described as conformably over-
lying gneiss, is in some places an intrusive syemnite, in others true
eranitic eneiss, but rising wp in nearly vertical masses with a strike
at nght ‘angles to the beds on which it has been said to rest. This

* Tt seems to be the rock thus described: “ Another prominent variety [of
gneiss] exists in a rock almost entirely composed of compact felspar and quartz,
arranged, not in distinct concretions, but, on the contrary, so closely connected
that their linear position can only be detected after atmospherical agents have
partially abraded the felspar. This remarkable gneiss forms some hills on the
south side of Loch More.”—Cunningham, Geog. of Sutherland, p. 77.

t In the geological map published in No. 62 of the Quart. Journ. Geol. Soc.
(May 1860), a broad band of “upper quartz-rock” is laid down in this region.
Tt is rather remarkable that these same rocks, now described as quartz-rock, were
quoted as a true overlying gneiss both by Macculloch and Cunningham. As
stated in the text, the rock is gneiss (but not overlying) or a syenite.

~

1860. | NICOL—N.W. HIGHLANDS, — 95

is well seen on the south side of Loch Glen Coul, where the quartzite,
which, only one or two miles south, expands into the great mountain-
group of Assynt, has been denuded almost to a single bed.

The section (fig. 7) of the northern side of Glasven shows the
true structure very clearly. The low hills on the west, near Kyle

Fig. 7.—Section of Glasven.

Ferry-na- Loch-na- Corry
cairn. Ganvich. Derg. Glasyen.

i

1
Nees
Nez

wee : - = P d S
an a a ie a
c\. Quartzite. 6. Red sandstone. a. Granitic gneiss.
aa. Gneiss with hornblende. s. Syenite.

Sku Ferry and Unapool, consist of gneiss and hornblende-rocks, the
strata often at very low angles (dip 12° N. 15° EK). ‘They are
covered by red sandstone, stretching south, in a broad terraced
valley, up into the corries of Queenaig. This valley is bordered on
the south-east by a precipitous cliff of quartzite, formed by a
great sheet of rock, which, sloping down from the summit of
Queenaig, folds over on the south to Loch Assynt, on the north to
Loch Glen Coul. The quartzite is well seen on the west side of
Loch-na-Ganvich, where the burn from the lake has almost cut
through the cliff in a deep ravine, and forms a picturesque waterfall
within a few yards of its exit*. The quartzite dips at 10°, to S..
53° E., apparently below the ridge of Glasven, hitherto represented
as entirely consisting of quartzite. The east side of the lake, how-
ever, I found was syenite, intermixed with nearly vertical masses
of granitic gneiss running N. 10°-15° W. ‘This rock forms the
whole north side of Glasven as tar back as the tarn of the Corry
Derg. The high bare cliffs on the south-east of this small lake
exhibit a beautiful section. The northern extremity consists of the
syenite, overlain on the south by undulating beds of quartzite’.
This rock forms the summit and southern slopes of Glasven; but
the syenite passes below and reappears on the other side of the
mountain. I have again found it in the inner corries of Ben
Uarran and Ben More; so that it probably forms the axis of the
whole range of mountains. From the Corry Derg it extends north
to Cnoc-na-Craig-Ganvich and the head of Loch Glen Coul, where

* We have here, therefore, a miniature of the phenomena of Niagara and the
American lakes. The erosive action has only to proceed a few yards further in
order to drain the lake ; but from the extreme hardness of the quartzite this may
ao a very long period.—See Sir C. Lyell’s Travels in North America, vol. 1.
pp- 29-46. ‘

t The little tarn is shut in on the north-west by moraines or glacier-mounds.
These on the north, opposite the syenite cliff, are entirely composed of syenite
boulders ; on the south, where the cliff is quartzite, of quartzite boulders, with:a
mixed group between. : :

‘ig. 8.—NSection of Assynt.

W.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 5,

the granitic gneiss intermixed with
syenite-veins is seen stretching away
to the east, below the quartzite-beds
of Ben Uie and Ben Uarran, and con-
tinuous with the gneiss of central
Sutherland. Nothing can be more
striking than the contrast between the
dark-grey gneiss and hornblende-rocks
forming the north-east base of these
mountains and the almost horizontal
beds of brilliant white quartzite, which
rest upon them for miles.

Assynt.—The structure of the Assynt
region is represented in the next sec-
tion (fig. 8), extending from Queenaig
on the west to the south-east declivities
of Ben More. The middle of the sec-
tion shows the strata as seen on the
north shore of Loch Assynt and in
Stronchrubie ; but im the background
I have sketched-in the northern range
of mountaing connecting Queenaig and
Ben More, showing the continuity of
the quartzite round the whole lime-
stone-plateau.

The first formation, on the west, is
the gneiss (a) intermixed with veins of
granite and syenite. It is covered by
red sandstone (6), beautifully seen in
the western declivities of Queenaig,
and,this by the quartzite (c’) sloping
down from the summit of the mountain
in vast, almost unbroken sheets. As
well seen in Skiag Burn, the dip is
about 10°, and thus probably uncon-
formable to the red sandstone below,
though the great faults intersecting
the mountains and the protrusion of
igneous rocks render this fact less
certain than I formerlythought. Above
it come the fucoid-beds (c’), and over °
them the limestone (d), forming the
whole low ground north of Loch
Assynt, from Skiag Bridge by Stronch-
rubie to the foot of the Ben More
mountains. This limestone is the
highest bed in the series, being every-
where troughed by the quartzite. As
this fact is of great importance, and
as it has been affirmed that an upper

Strath of Oykill.

Strathan Water.
mM. Loch Maolack Corry.

s. Syenite.

Ben More.

(The gneiss of Queenaig

has granitic and syenitic veins.)

Stronchrubie.

Inch-na-
a. Gneiss.

ge. Assynt. Damff.

Skiag Loch

Brid

4, Red sandstone.

el. Quartzite.

Loch Assynt.

d. Limestone.
c, Fucoid-beds.

Queenaig.

1860. | NICOL—N.W. HIGHLANDS. 97

quartzite and limestone occur in this region, a few confirmatory
facts and sections must be noticed.
_ In ascending the road from Skiag Bridge towards Kyle Sku, the
fucoid-beds and limestone may be seen resting on the quartzite,
almost to the summit of the ridge. Before reaching the foot of
Glasven, however, they thin out, and the quartzite of that mountain
and of Queenaig form one continuous mass, as shown in the section.
That the quartzite of Glasven does not overlie the limestone is
further proved by no trace of limestone being seen in the Corry
Derg (fig. 7, p. 95), where the syenite brings up the bottom beds,
or between the quartzite and gneiss in the noble sections exposed on
the north-east side of that mountain, formerly described.

The same thing is shown by the section from Loch Assynt near
the School-house, in a N.N.E. direction across Cnoc-an-drein.
Close to the lake the quartzite is seen cropping out below the lime-
stone, which forms all the declivity of the hill, and dips to EK. 25° to
30° N., at angles ranging from 20° to 40° or more. This diversity
of dip is caused by the intrusion among the strata of irregular veins,
or lenticular-shaped masses of trap, of which I enumerated not
fewer than eight or ten. Near the top of the ridge the quartzite
appears to rest on the limestone, but is separated from it by veins of
green trap and of dark clove-brown felspar-porphyry. The quartz-
ite (Pipe-rock) dips first E. at 25° to 35°, and then higher up on
Cnoc-an-drein rises to 75° to 80°, at length becoming vertical, with
a N.N.W. strike, having clearly been forced up by the intrusion of
the syenite (shown at s in figs. 7 & 8).

The inferiority of the quartzite to the limestone is even more
clearly seen in the Poulan-drein Burn, at the south-east end of Cnoc-
an-drein ; it may also be seen along the whole valley of the Traligill
River, almost to the Bealach at the foot of Ben More. Everywhere
the limestone, which in the plateau of Stronchrubie on the south
side of the stream dips towards these mountains, is found to form
a synclinal axis, and on the north side to dip away from the quartz-
ite. The only obscurity in the sections arises from the synclinal
fold in the limestone being conjoined with a great fault in the quartz-
ite, which is thus brought up in enormous crushed masses, so broken
that the lines of stratification can hardly be detected*: this is
especially seen near the foot of Coniveal; but in no place have I
observed the limestone dipping below the quartzite of these moun-
tains.

In the line of the section no such obscurity exists. Immediately
to the east of Loch Maolack-Corry, well known for its Gillaroo trout,
the Stronchrubie limestone, continuous throughout, rises up into a
hill, and is seen very distinctly dipping at 40°, to W. 40° N., in

* This peculiar combination of faults with synclinals (or what may be named
a ‘“‘faulted-synclinal”’) is very common in Sutherland. It has probably been
caused by the refractory nature of the quartzite, which was more easily broken
than bent. To the same cause we may ascribe the frequent combination of a
crush (or broken and brecciated condition of the rock) with one or both of these
faults and synclinals.

VOL. XVIIT.—PART I. H

98 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

slightly undulating beds. On the east side of this hill the limestone
rests on the red shales or fucoid-beds (¢’), and these in turn on the
quartzite (c'), dipping at 20°, to W. 40° N., and rising in great curved
beds to the top of the next hill. The section is so clear, and the
correspondence of the deposits so exact, that there can be no doubt
that this is the east side of the Queenaig synclinal. Still stronger
evidence of this fact may be obtained by tracing the quartzite along
the shore of Loch Assynt and up the Stronchrubie valley*, every-
where dipping below the limestone, till it turns round its southern
extremity and rises up into Brebag. From this mountain the
quartzite may be followed along the bare ledges of rock north to
Ben More, and thence, as shown in the section, round till it again
joins that of Queenaig.

A more interesting confirmation of this peculiar structure of the
Assynt district (the highest of its formations, filling the bottom of
the valley) is furnished by the drainage of its waters. Almost all
the streams from the lofty north-eastern mountains, from Brebag,
Ben More, and Ben Uarran, on reaching the synclinal line in the
limestone, fall into swallow-holes and disappear for a considerable
space. The whole moor is dotted over with round pits, some dry,
some filled with water at the bottom, through which the drainage is
effected. In some places deserted river-beds, only occupied by the
water in rainy seasons, are seen; in other places the subterranean
torrent is heard rolling along at the bottom of a deep dark cave.
Now all this underground drainage is directed towards Loch Assynt,
the centre of the synclinal, proving that the strata dip to this poit,
and not north or east below Ben More or Brebag. The water de-
scends through the limestone to the quartzite, and is again thrown
out on the surface by this impervious stratum, often in very copious
springs?.

There is thus, in this place, no “ upper quartz-rock”’ resting on
the Stronchrubie and Assynt limestone, and the hills referred to this
newer formation clearly consist of the quartzite below the limestone,
brought up over an anticlinal. Singularly enough, too, some of
these so-called “‘ upper ”’ or ‘‘ newer quartz-rocks”’ are even an older
formation than the lower quartzite. When examining Canisp and
Queenaig, I was struck by the peculiar aspect of some of the hills on
the eastern side of Stronchrubie, usually classed as quartzite. From
their reddish colour I thought that they probably consisted of felspar-
porphyry, like that of Loch Borrolan; but on examination I found
that they were formed of red sandstone, identical in character with

* In my former paper (Quart. Journ. Geol. Soc. vol. xiii. p. 25) I stated that
the Stronchrubie limestone and the underlying quartzite had ‘probably been
brought up by a fault.” Several faults in the line of that section are well seen
in the face of the Stronchrubie cliff; but, as shown in the present section, the
limestone and quartzite are brought up rather by undulations in the beds and
the general rise of the synclinal than by these faults. Compare Quart. Journ.
Geol. Soc. vol. xvi. p. 221 (note f).

t I estimated the flow of the “‘ Remarkable Spring” above Stronchrubie at
7000 gallons per minute, after some weeks of dry weather.

1860. ] NICOL—N.W. HIGHLANDS. 99

that of Queenaig and Suilven. In the corries of Ben More similar
beds occur, resting on gneiss or mica-slate (as shown in the section) ;
and there can be no doubt that this is the true western Red Sand-
stone (‘ Cambrian” of Murchison) brought up in the centre of the
so-called “ upper quartz-rock,” and that the synclinal is thus com-
plete in all the formations from the upper limestone to the lowest
gneiss.

The eastern extremity of the section shows the true structure of
Ben More, as exposed in the wild corries round the Dhu Loch More.
Granitic gneiss and mica-slate, with intrusive igneous rocks, form
the nucleus of the mountain, throwing off the quartzite all around,
as from a great centre of elevation. Further west an enormous
mass of beautiful binary granite rises into a group of rugged moun-
tains, quite unlike the quartzite with which they have hitherto been
confounded*. Taken in connexion with the Loch Borrolan por-
phyry, with which it is probably continuous, this granite must pro-
duce most powerful disturbance along the south-east border of the
quartzite ; and we can easily understand how observers who ignored
or overlooked its existence should mistake the true relations of the
stratified rocks it has affected.

Loch Ailsh Section.—lt is, again, affirmed that in the vicinity of
Loch Ailsh and the higher part of Strath Oykill, the “ upper quartz-
rock” forming the Assynt mountains “is overlain by a second zone
of limestone,” and both “ conformably surmounted by upper mica-
ceous, chloritic, gneissose, flaggy strata... for several miles across
the strataz.’’ My examination of the locality last summer (1860) by
no means confirms these views. The ‘“ upper quartz-rock ” is simply
the continuation of the quartzite of Brebag and Canisp, and the
“second zone of limestone” merely the repetition, in a denuded
form, on the other side of the anticlinal, of the limestone of Stron-
chrubie and Assynt. Any slight change in the colour or character
of the strata is readily accounted for by the intrusion of the red
porphyry of Loch Borrolan, which probably at no great depth under-
lies the rocks shown in the section (fig. 9).

This section begins on the west, at Cnoc Chaorinie, with a hard
reddish or clove-brown hornstone-porphyry (a) with distinct cry-
stals of felspar, but probably only a semifused mass of the quartzite.

* Tn justice to Mr. Cunningham, it must be stated that the greater portion of
these granite mountains lie in Ross-shire, and thus beyond the limits of his map.
Tt In the Quart. Journ. Geol. Soe. vol. xvi. p. 282, it is stated that “no ig-
neous rock has yet been observed to be associated with the lower quartz-rock of
Assynt ;” and that the “large crystalled porphyry ” of Canisp may be considered
‘for the present to be characteristic of the Cambrian age in the North-western
Highlands.” Jn 1859, I found that this very beautiful porphyry not only breaks
though the quartzite of Canisp, but forms a mass more than a mile in diameter
in the same “ lower quartz-rock,” within a few hundred yards of the inn of Inch-
na-Damff. It is thus of later date than either the Red Sandstone or Quartzite,
and is one of those powerful agents affecting the relations of these and the other
strata which have hitherto been overlooked.
{ Sir R. I. Murchison, “Supplemental Observations on the North of Scot-
land,” Quart. Journ. Geol. Soc. vol. xvi. p. 228.
H 2

100 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

It passes up into great masses of red hornstone or hardened quartzite
(c') mixed with fragments of limestone, and dipping very irregu-
larly at about 20°, to E.10°N. A true quartzite succeeds, dipping

Fig. 9.—Section near Loch Ailsh.
Cnoc-Chaorinie. Alt-Ellag.

cf Ce @
. Quartzite. c*. Fucoid-beds. a. Chlorite-slate and gneiss.
x, p}, p*. Porphyries.

at 25°, to E. 10° S., and overlain by irregular masses of red lime-
stone. Red felspar-porphyry (p’) follows, then quartzite, dipping
at 35°, and then the fucoid or slaty beds (c*) intercalated with red
limestone and quartzite, and dipping at 43° to 30°, to E. Passing
over a low ridge, the next beds seen are hardened quartzite, dipping
at 50°, to E. 20°S. A small stream descending from the hill marks
a line of fault; and beyond it beds of chlorite-slate, beautifully econ-
torted, and resembling marbled paper on the cross-fracture, oecur.
A second vein of red felspar-porphyry (p*) follows, and then fine-
grained quartzose gneiss, dipping first 20°, to E., and then 40°, to
E. 40°8. From this point to Alt-Ellag (a distance of half a mile),
the rocks are fine-grained slaty gneiss in undulating beds, but the
dip gradually falling to 23°, 18°, and 16° at the Bridge. The same
fine-grained, micaceous, undulating gneiss continues down Strath
Oykill to Rosehall, but in all the lower part of the valley, beyond the
influence of the porphyry and granite on the west, has a persistent
N.W. strike and 8.W. dip (dip 45°-50°, to 8. 15°-25° W.*),

The facts just stated leave little doubt as to the true relations of
the beds in this section. The only obscurity arises from the strata
being much concealed by soil and grass, and only visible at intervals
where they crop out on the surface, and, from the repeated intrusion
of igneous masses, modifying the usual aspect of the rocks. The
lower part of the section is evidently the quartzite hardened and
altered by contact with igneous rocks: the centre is no less plainly
the fucoid-beds, intermixed with some thin beds of red limestone
and quartzite. Over these, had the series been complete, the dark-
blue or grey limestone ought to have appeared, but is wanting in
this place; then follows the gneiss, probably crushed out of its do-
minant north-west strike in the lower Strath Oykill by the intrusion
of the western porphyry and granite. The remarkable change in
the dip on both sides of the line of junction proves the existence of
a fault; but the absence of the limestone is specially fatal to the
opinion that there is here “‘ conformable upward succession.” This
absence is the more remarkable from its occurrence in full strength
at Elphin to the south, and also on Loch Ailsh to the north. I fol-
lowed the limestone along this north line till it was cut out by the

* See also the dips on Cunningham’s map.

1860. | NICOL—N.W. HIGHLANDS. 101

granite, but I could find no place where it is seen to dip below the
gneiss. Even in the deep ravines of the Alt-na-Caillich, close to the
line of junction, where the eastern gneiss is exposed for a thickness
of some hundred feet, I could discover no limestone below it. This
is the more remarkable as, from the enormous protrusion of igneous
rocks on the west, some such anomalous features might have been
expected to occur*. :

Elphin and Craig-a-Chnockan.—Having now noticed all the sec-
tions adduced in proof of the eastern gneiss overlying the limestone
and quartzite, I shall pass more rapidly over some others in the
southward extension of the lne of fracture, though not less in-
teresting and instructive. To the south of Loch Borrolan and the
Strath Oykill road the country is flat and obscured by moss and drift,
but the limestone and quartzite appear to be thrown west to the east
end of Loch Urigill. The whole eastern anticlinal of Ben More and
Brebag has in this region been swept away, and the line of junction
is in the continuation of the synclinal passing through the Gillaroo
Loch. So extensive has been the denudation of the overlying quartz-
ite and limestone that the gneiss is almost continuous from west to
east. True granitic gneiss with syenite-veins is seen very distinctly
at the east end of the Camaloch, whilst, according to Mr. Cunning-
ham, gneiss also extends from the upper part of Loch Urigill into
the Cromalt Hills.

Round Elphin the limestone is very well seen, resting, as usual,
on the fucoid-beds and quartzite (dip 12°—15°, to E. or E. 10° §.).
These beds are very fully exposed for some miles, and their relation
to the eastern gneiss clearly shown in the precipitous cliff of Craig-
a-Chnockan, below which the Ullapool road passes. The section

Fig. 10.—-Section on the Ullapool Road, near Elphin.
W. Coulmore. E.

Craig-a-Chnockan.

=< SSS

d. Limestone. c, Fucoid-beds. c', Quartzite. 6. Red sandstone.
a. Gneiss. - x. Granitic vein.

fig. 10 shows the structure of this place. In the west, Coulmore
consists of the Red Sandstone. The valley below is quartzite, ex-
tending up to the cliff of Craig-a-Chnockan. In the line of section it
dips 12°—15°, to E. 40°S., and is covered by the limestone. Further
east the limestone rises up and thins out, and the quartzite comes

* The section fig. 5 (p. 223 in Quart. Journ. Geol. Soe. vol. xvi.), though said
to occur to the east of Alt-Ellag (where I am not aware that any quartzite or
limestone is to be found), probably refers to this locality ; but I could observe
no place where the beds rest connectedly on each other as there represented.
Even in it, however, the sequence is broken by “ hornstone-porphyry ;” and the
“gneissose limestone” is perhaps also an intrusive rock. ‘The absence, too, of
the fucoid-beds and limestone inttheir normal form is opposed to any regular
upward succession in that section.

102 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

to the surface, followed (still to the east) by fine-grained gneiss,
much curved and contorted, but dipping at 35° to 50°, to S. 5° W.
In this line a thin vein of granite or syenite, like that on Loch Erri-
boll, intervenes. Further south, on the Ullapool road, the line of
junction intersects the front of the vertical cliff, and the strata are
well exposed. The quartzite, dipping at 5° or 6°, and covered by
the fucoid-beds and limestone, comes within a few yards of the gneiss.
A thick, strong bed of the quartzite then dips down at 12°, as if
below the gneiss, whilst the thinner fucoid-beds above are curved
and fractured and the limestone broken suddenly off. The dark-
coloured, thin-bedded gneiss dips at 20°, and is traversed by innu-
merable fissures, filled with thin lines of the granitic rock, running
up the face of the cliff, from which, a little to the south, a large
mass of trap protrudes. Had the strata been less clearly exposed,
the gneiss might have been supposed to overlie the quartzite; but
the fracture and contortion of the beds, seen even in hand-specimens,
and particularly the manner in which the limestone and fucoid-beds
are cut out, prove that there is, in this place, not ‘“ conformable
upward succession,” but a line of fault with powerful lateral com-
pression.

Loch Broom.—The next point to the south where the rocks are
well seen is the vicinity of Loch Broom, described in my former
paper*. As there stated, the quartzite is cut off from the gneiss by
a thick bed of intrusive rock, in some places a felspar-porphyry, in
others near the limestone inclining to serpentine, but generally
identical in character with the rocks in the same position in the
previous sections. This summer (1860) I again visited Loch Broom,
but saw little to add to my former memoir, except that the porphyry
or igneous rock is more extensive than represented in the sections,
and, rising up in a wider mass below, separates the eastern gneiss
more strongly from the quartzite. I must also call attention to the
fact, exhibited in the sections, that, whilst on the north shore the
series of the quartzite group is complete, on the south side of Loch
Broom the limestone above has been entirely cut out.

Loch Maree and Gairloch.—tIn my former paper I described some
sections in the vicinity of the Gairloch and Loch Maree. I have
since examined the mountains round the upper portion of that most
beautiful lake, and the line of junction between the quartzite and
gneiss with some care; and the section (fig. 11, p. 104) shows the facts
as seen on the north side of the loch: In the west there is, first, the
red sandstone (6), dipping west at a low angle, as seen near Pol Ewe
and the Gairloch. Then follows the gneiss, as formerly stated, often
a fine-grained grey rock with intercalated beds of mica-slate, in Ben
Lair, with hornblende-strata. Near the head of the loch the red
sandstone cone of Sleugach rises above a basis of gneiss, forming one
of the grandest mountains in this truly mountain-region. The
eneiss, generally red or grey and highly crystalline, where seen
below the red sandstone dipped 70°-80°, toW. 20°S., and hence has

43
* Quart. Journ. Geol. Soc. vol. xiii. (1856) p. 18-24 and figs. 1 & 2.

1860. | NICOL—N.W. HIGHLANDS. 103

a N.W. strike. Where it meets the red sandstone the surface is
very rugged and uneven, and the beds above are often, as noticed on
the Gairloch, a coarse angular breccia. The red sandstone dips 15°,
to §. 33° E. In the mountain, east of Sleugach, and separated from
it by a deep ravine, the red sandstone is covered by the quartzite,
which continues along the summit of the ridge to Glen Laggan.
The red sandstone, however, forms the foot of the hill to the head
of the loch; but further up a great mass of igneous rock (s) (a fine-
grained syenite, or rather diorite) forms the base of the hill, covered
by broken masses of quartzite and limestone. In the valley of the
Laggan the limestone (d) has been quarried in several places, dip-
ping to E. 20° S., but much altered by the diorite (s), which forms
a wide mass, running for several miles along the valley. The other
side of the valley consists of grey granitic gneiss (a), in some places
more quartzose, in others fine-grained and micaceous, and dipping
15°-30°, to E. 30°-40°S. In the low ground, however, near the
mouth of the glen, grey granitic gneiss occurs, dipping at 60°-70°, to
KE. 45° N., and thus with a true N.W. strike, though on the east
side of the fault and of the quartzite*. In this place, though the
formations are only separated by a deep and narrow valley, yet the
quartzite is nowhere seen dipping below the gneiss on the east, nor
the gneiss resting on the quartzite on the west.

In the low ground near Kinloch Ewe, the gneiss is seen in the
bed of the river near the inn, dipping 10° to 8. 45° K., and about a
quarter of a mile west the red sandstone forms some low rounded
knolls. The intervening space is thickly covered by detritus; but,
from the dip of the beds, the red sandstone here is probably in con-
tact with the eastern gneiss, the limestone and quartzite having
been entirely denuded. The quartzite, sloping down from Ben Ey,
covers the red sandstone on the south, but at the foot of Loeh Clair
is again thrown out, so that the eastern gneiss and red sandstone are
brought into contact. The same relation also appears to occur in
the wild country towards Loch Carron. Anyhow we find in this
region that the limestone, forming the upper portion of the quartzite
series, only oceurs in rare fragments, where left behind in the de-
nuding process, so that the phenomena are quite opposed to any
theory of continuous upward succession.

In regard to the relation of the quartzite and red sandstone in
this region, they seem to be generally conformable to each other. I
infer this, rather from the view of the two formations as exposed in
the mural precipices of the mountains, than from direct observation
on the beds. This general parallelism is very marked in Leagach,
one of the loftiest mountains on the west coast, and, as the appear-
ance is the same whether the hill is looked at from the north or
south, can hardly be a mere optical effect. In Ben Ey (a mountain
nearly as high, but more picturesque), the same parallelism appears,
and is the more striking from both the red sandstone and quartzite

* It may thus be regarded as the other side of the anticlinal to the beds seen
under the ved sandstone of Sleugach.

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PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

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1860. | NICOL—N.W. HIGHLANDS. 105

having been tilted over towards the line of fault on the east, as shown
in the sketch* fig. 12.

Fig. 12.—Section of Ben Ey and Leagach. Seen from the north.

c. Quartzite. 6. Red sandstone.

Loch Torridon and Loch Carvon.—Immediately south of Loch
Maree and the Gairloch lies the wild unfrequented district of Loch
Torridon. On the shores of this most magnificent sea-loch, and in
the lofty mountains that surround it on every side, there is some of
the grandest scenery in Scotland, and at the same time some of the
most instructive geological sections. The whole structure of the
mountains is clearly exposed in the naked precipitous walls of rock,
built up, layer above layer, in the most majestic piles of masonry.
How geologists could traverse this region, and yet believe that the
great Red Sandstone formation of Applecross and the West Highlands
was superior to the quartzite, is hard to understand; and yet this
was regarded as an established fact up to the publication of my paper
on the N.W. Highlands in 1856.

The lowest formation is, as usual, the gneiss, well seen on the
narrows near Sheildag, where its dip is N.E., and commonly at a
considerable angle. It rises to a height of 2000 to 3000 feet in Ben
Ailigin and the Gairloch mountains, but is in most places hidden by
the red sandstone. On the lower loch the red sandstone generally
dips west at 8° or 10°, but often higher near the outer headlands.
In many places it seems almost horizontal, as in the lofty moun-
tain of Leagach, where it is covered apparently in conformable
superposition by the white quartzite. Onthe upper Loch Torridon
the dip changes to the east, and then retains this direction through-
out. As shown in the section (fig. 13) of the mountains east of
Loch Torridon, it is still overlain by the quartzite. In this most
remarkable section, the red sandstone, always dipping to the east,
and covered by its capping of quartzite, is again and again brought up
by faults; and this not only on the summits of distinct mountains,
but no less than five times in a single continuous ridge. Had only
a surface-view been exposed, as each fragment of quartzite seems to
dip below the next one of red sandstone, it might have been supposed
that the rocks alternated with each other ; but no such mistake can
be made in this place, as the true structure of the mountain, to a
depth of some hundred feet, is clearly exhibited in the vertical escarp-

* This rough sketch, taken from the plateau on the north, shows only about
half the true elevation.

106 PROCEEDINGS OF THE GHOLOGICAL SOCIETY. [ Dee. 5,

ments of the mountain, and repeated with equal distinctness in the
corresponding precipices on the other side of the valley. It is im-
possible to give verbal details; but the figure, imperfect as it un-
avoidably is, represents the facts more distinctly than words. It is
clear that the quartzite is mere fragments of the upper formation,
brought down repeatedly by faults, and in some cases even forced in
below the inferior red sandstone by enormous lateral pressure. This
very clear natural section thus tells us the structure of the N.W.
Highlands, and the true nature of those apparently anomalous
sections which have puzzled observers in other parts of the line of
junction.

The most critical point of the section is at the eastern extremity,
where the red sandstone and quartzite meet the gneiss or, rather,
mica-slate. Near this point the quartzite, still resting on red sand-
stone, is thrown down some hundred feet below its former level.
Repeated slips take place, still further depressing the quartzite and
red sandstone, the latter dipping at about 15°, until near the line of
junction, where both the quartzite and sandstone dip at 33°, to 8.
95° KE. An irregular, but nearly vertical, line of fault here separates
them from the mica-slate, dippimg on the whole at 40° or 50°, toS.
or 8.E., but in some parts ranging from 15° to 60°, and dipping in
various directions from N.E. to S.W. It forms but a mere coating,
as it were, on the front of the hill, and is in part intermixed with
compact syenitic rocks, which may explain the irregularity in the
dip and direction of the beds. In this place, therefore, there is no
overlap of the gneiss on the quartzite, but the two formations meet,
end to end, along a line of fracture. It is also noteworthy that in
this section the red sandstone does not thin-out before the quartzite,
as in some of the northern localities, -but comes up almost into con-
tact with the gneiss.

Another section in the hills between Loch Carron and Loch Kees-
horn (fig. 14) exhibits the same relation even more clearly. In this

Fig. 14.—Section near Loch Carron.
Roustag. Meal-na-Damb.

cl. Quartzite.
a. Talcose or chloritic schist, with granitoid veins.

place the quartzite, resting on the red sandstone, rises into some
lofty mountains. Near the line of junction it dips at 50° to 60°, to
E. 20° §., but is fractured and broken, and small fragments of the
limestone are involyed between it and the tale or chlorite-slate.
This rock is much intermixed with veins of red granitoid matter,
and dips very irregularly at angles of 20° to 30°, to E. 15° to 45° §.,
but in part at low angles nearly north. A small stream, running

1860. ] NICOL—N.W. HIGHLANDS. 107

down the side of the hill, along the line of junction, has fully ex-
posed the connexion of the two rocks, but in no place could I find
the talc-slate resting on the quartzite. Had the beds been continued
in the dip, so as to pass below the slate, this could scarcely have
failed to be visible.

In my former paper there is a section of the Loch Keeshorn lime-
stone*. Ihave since examined the district more carefully than I
was then able to do. I have now ascertained that the limestone
rests on the quartzite, which in one place dips at 15°, to 8. 40° E.
The limestone is, as usual, more broken and irregular, but near the
bridge to Applecross it dips at 64°, to E. 8° N. The talc-slates on the
east have a dip of 20°, to E. 30° N.; and, on the whole, lower angles
than those given in my former paper seem to prevail in these beds.
Granulite and hornblende-rocks, however, abound near the line of
junction ; and J was still unsuccessful in finding any point where the
tale- or mica-slates overlap the limestone or quartzite. I have now
no doubt, from the facts seen at the junction in other places, that the
limestone and tale-slate are divided by a line of fault. The occur-
rence of the limestone in this position, though quite analogous to
what is seen in Assynt, is very important. It lies in a low valley
at the foot of the red sandstone hills of Applecross, more than 2000
feet high, and, as its regular position is above the quartzite, it must
haye been thrown down from fully 3000 feet. It must at one
time also have been far more widely distributed; fragments of it,
some only a few feet or yards in diameter, being found in many
places, let in (as it were) along the line of junction of the quartzite
and crystalline schists. There is thus evidence of a most enormous
amount both of disturbance and denudation in this region; and also
proof that, where the quartzite meets the talc-slates or gneiss, with-
out the intervention of the limestone, whatever may be their appa-
rent relations, there cannot possibly be a true conformable upward
succession.

South of Skye.—The section of the southern part of Skye given in
my former paper (fig. 7, p. 31) offers similar proof that the red sand-
stone does not dip under, but rests unconformably on, the eastern
gneiss, and this gneiss dipping 8.E., and identical in mineral cha-
racter with that of the mainland. The red sandstone dips W.N.W.,
and is clearly continuous with that of Applecross and the North-west.
The section is so clear and decisive that I can do nothing more than
refer to the description in my former paper ft.

General Considerations.

The sections now noticed, at short intervals along the whole line
of junction from north to south, seem quite decisive of the true re-
lations of the quartzite and eastern gneiss. They have not been
selected as more favourable to my own views than others that might

* Quart. Journ. Geol. Soe. vol. xiii. p. 29. fig. 6.

t Quart. Journ. Geol. Soe. vol. xiii. p.31. Inthe sketch-map. in vol. xv. pl. 12,
this underlying gneiss is coloured and lettered the same as the so-called over-
lying gneiss in Sutherland.

108 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

have been chosen, but are those brought forward as the proofs on
which the opposite theory is founded; yet in not one of them have
we found that regular continuous upward succession which this
theory requires, but in every one of them irruptions of igneous in-
trusive rocks, and other indications of faults and disturbance, de-
priving them of all weight as evidence of regular order. Here,
therefore, I might have left the question, satisfied with this appeal
to special sections; but there are a few more general facts, leading
to the same conclusion, which require a short notice. In order to
perceive the full force of these facts as bearing on the present ques-
tion, it must ever be kept in mind that this region has undergone a
most enormous amount of denudation—strata of at least 2000 to
3000 feet in thickness having in some places been swept away from
the surface ; consequently, if there be here a line of conformable
overlap, all the beds that dip east (the so-called “ upper gneiss,”
the limestone, and quartzite) must have originally extended much
further to the west.

First. The mode of distribution of the rocks is altogether incon-
sistent with the hypothesis that the eastern gneiss overlies the red
sandstone or quartzite. The red sandstone, with a width from east
to west of thirty to fifty miles, is seen in innumerable places—at
Stornoway, Cape Wrath, Assynt, Gairloch, Skye, resting for miles
in all directions on the gneiss. So also the quartzite, with a breadth
of ten or twelve miles, is everywhere clearly seen to rest on the red
sandstone. Mile after mile, from north to south and east to west,
from mountain-top to mountain-top, from valley to valley, this rela-
tion may be traced. And thus also it is with the limestone, though
this formation is now of such limited dimensions. In every locality
where it occurs—Durness, Erriboll, Loch More, Assynt, Ullapool,
Loch Maree, Loch Keeshorn, it is seen resting on the quartzite.
This relation can be traced round and round isolated masses of the
limestone, and across synclinal basins of miles in extent. But how
does it stand with the next step in the series, the so-called ‘“ upper
gneiss” or mica-slate? This gneiss extends for fifty or a hundred
miles to the east, and, we are told, conformably overlies the quartz-
ite or the limestone, for a hundred miles from north to south; and
for what distance to the east or west of the line of junction has this
overlap been observed? Nowhere for more than a few feet, or yards,
at one or two widely separated intervals, has this overlap ever been
even alledged to occur. We seek in vain for any isolated portion of
mica-slate resting on quartzite or limestone, on the west of this line
of supposed overlap; and it is as fruitless to ask which of the thou-
sands of lofty gneiss-mountains on the east reposes on a basis of
these so-called older rocks. Such a thorough diversity in this step
in the series from all those that precede, and from all the known
relations of overlying beds in other countries, proves that here no
such overlap takes place.

Second. The diversity in the strata brought into contact with
the eastern gneiss proves that the line of junction is along a fault,
and not one of conformable upward succession. Where a series of

1860. | NICOL—N.W. HIGHLANDS. 109

beds rest conformably on each other, no amount of denudation can
ever alter their order, or cut out one or two members of the series ;
but along a line of fault the case is just the reverse: always, as
denudation proceeds, older and older beds will be brought to the
surface, and thus into contact with the gneiss. This will be readily
understood from the diagram fig. 1. As drawn, the limestone d is
shown in contact with the eastern gneiss a. A small amount of
denudation would bring first the fucoid-beds c*, then the quartzite
c', the red sandstone 6, and even the western gneiss, into contact
with the eastern gneiss. On the other hand, in the contrasted
section (fig. 2, p. 217) in vol. xvi. of the Journal of the Society, it
is evident that no amount of denudation could ever bring the
eneissic flagstones d? on the east into contact with the lower lime-
stones ¢° or quartzite c’, and still less with the Cambrian sandstone b.
But my sections show (and the fact cannot be disputed) that in
some places the limestone, in others (and more often) the quartzite,
in others the red sandstone, thus come into contact with the gneiss.
As a marked instance, I may refer to Loch Maree, where, in less
than a couple of miles, all these relations may be seen, as denudation
has been more or lessextensive. In the hill on one side of the valley
it is hmestone, in the low ground in the centre the red sandstone, and
then, on the other side, the quartzite. How “conformable upward
succession” can explain such relations I cannot comprehend.

Third. That there is here a line of fault, and not of conformable
overlap, is proved by the nature of the formations. Though along
the line of fault, and especially where the disturbance has been
most violent, the quartzite is often much hardened and semifused,
still it is a decidedly fragmentary, granular rock. The gneiss or
mica-slates, said to rest on it, are no less distinctly crystalline in
structure. This is true even of the finest-grained of these strata.
Now, before we can accept the theory of superposition, this fact must
be explained. That a truly crystalline metamorphic rock should
rest on deposits, thousands of feet thick, of unaltered sandstones
and limestones with fossils, is so improbable, so contrary to all the
established principles of geology, that nothing but the most un-
doubted evidence and the failure of all other methods of explanation
would justify us in admitting the fact. In the Alps, where such
superposition of crystalline on unaltered strata is seen, the most
distinguished and experienced geologists have found it “ necessary to
admit that the strata had been inverted, not by frequent folds. .. .
but in one enormous overthrow, so that over the wide horizontal
area, the uppermost strata, which might have been lying in troughs
or depressions due to some grand early plication, were covered by the
lateral extrusion over them of older and more crystalline masses*.’’

* Sir R. I. Murchison, “ On the Structure of the Alps, &c.,’’ Quart. Geol. Journ.
vol. y. p. 248. I need hardly say that no locality is known to me in Scotland
where the crystalline strata overlie the limestone or quartzite in the clear manner
shown in the section (fig. 28, p. 246) to which the above extract refers. The

phenomena in some parts of Sutherland are more closely represented by fig. 4,

p- 182, fig. 16, p. 203, and fig. 19, p. 209, of the same valuable and instructive
memoir.

110 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dee. 5,

A comparatively very small amount of inversion and extrusion of
older crystalline masses will suffice to explain any of the Scottish
sections, even as drawn and described by the advocates of an over-
lying “younger gneiss.” That such inversion and extrusion of
older masses on younger (though not of gneiss on quartzite) do
occur in this region of Scotland, and close to this line of fault, is
shown in the section of Sailmhore (fig. 13, p. 104); and, until some
rational theory is produced of the mode in which an overlying
formation, hundreds of square miles in extent and thousands of feet
in thickness, can have been metamorphosed, whilst the underlying
formation, of equal thickness and scarcely less in extent, has escaped,
we shall be justified in admitting inversions and extrusion equal to
those in the Alps.

Strike of the beds.—Two general facts have been adduced in proof
of the diversity of age of the gneiss on the west coast of Sutherland
and that forming the interior of the country—the diversity in strike
and in mineral character. Now it is evident that the relative age of
the gneiss in these two regions is an entirely different question from
the question whether or not the eastern gneiss overlies the quartzite.
[have more than once stated that the gneiss of Scotland probably be-
longs in part to distinct geological periods, and have specially pointed
out “ the great tract of gneiss with associated quartzite and limestone,
stretching from Aberdeenshire through Perthshire to the Breadal-
bane Highlands of Argyleshire, as a newer formation*.” And such
newer beds might also occur in Sutherland and yet not overlie the
quartzite. In regard to the strike of the gneiss, I mentioned in my
former paper that in the western region “its general direction was
to the N.W.,” whereas, as Macculloch had long before stated, m the
centre of the country it was more commonly “to the south-east-
ward +.” But this distinction is not universal. The mica-slate of
Far-out Head dips to the S.E.; and, as Mr. Cunningham shows,
the gneiss round Canisp and Suilven has also a N.E. strike, and a
sumilar strike with 8.E. dip is common in the south of the Lewis.
On the other hand, a N.W. strike prevails in Strath Oylall and the
lower part of Loch Shin, and in Ross-shire similar diversity occurs.
This sudden and entire change in the strike of the rocks in different
parts of the Highlands is, however, a very marked feature, and is
clearly connected with that peculiarity of structure exhibited by the
previous sections. The country does not consist of one large mass
of strata, but of fragments, irregular in form and of more or less
extent, and each subject to its own laws of position. They may be
well compared to the shoals of ice seen on a river-bank in spring,
each turned in its own direction, with little reference to the frag-
ments beside it.

There can be no doubt, however, that the country has undergone
a very general disturbance subsequent to the deposition of the

* Note explanatory of the Geol. Map of Scotland, pp. 2,3; and the Section
engraved on the Map. See also “On the Slate Rocks of Easdale, &c.,” Quart.
Journ. Geol. Soc. vol. xv. p. 110.

t Quart. Journ. Geol. Soe. vol. xiii. pp. 39, 37.

1860. | NICOL—N.W. HIGHLANDS. i

quartzite, throwing it over in large fragments to the 8.E., indepen-
dent altogether of the present strike or dip of the beds. This is
clearly shown on the west side of Loch Erriboll, where the quartzite,
with the inferior gneiss-plateau on which it rests, have both a dip
to the S.E. This is also true of the great plateau of gneiss on which
we must suppose the quartzite of Foimaven and Arkle, now dipping
at 20° to the S.E., to have been laid down in nearly horizontal
masses. So also on Loch Maree and Loch Carron, there is evidence
of the upturn of the formations in enormous fragments. Further
east, the same overthrow of the masses from the N.W. is evident in
the form of the hills and in the position of the newer formations of
the east coast. The cause of this most remarkable convulsion must
be sought in some more powerful agent than any of the masses of
igneous rocks now visible on the surface in this part of Scotland.
Mineral character.—The diversity in the mineralogical character of
the rocks has also been often alleged in proof of the overlap of the
eastern gneiss. Now it must be stated that, though Dr. Macculloch
coloured the whole of central Sutherland as gneiss, yet Mr. Cunning-
ham recognized that some portions of it were mica-slate ; and the same
distinction appears in subsequent maps. In comparing the gneiss of
the east with that of the west, such mica- and chlorite-slates must
of course bé set aside, though it is undoubtedly true that they are
quite as crystalline in texture, and as distinctly separated from
the true sedimentary formations, as the gneiss. In regard to the
gneiss itself, Mr. Cunningham, undoubtedly both a competent and
an unprejudiced observer, states that ‘‘the mineral characters of
both” (the eastern gneiss, which he believed to overlie the quartzite,
and the western, which underlies it) ‘are essentially the same*,”
and expressly affirms that “‘he has never found any indications of
mechanical action on its individual constituent minerals?.” It is
no doubt true that ‘‘ hornblendic varieties of gneiss are very cha-
racteristic of this formation in the west of Sutherland ¢;” but the
more usual kinds also occur, and in the Gairloch district its general
aspect “is a light or dark grey, finely granular rock, interstratitied
with beds of mica-slate§.”’ In Far-out Head, again, it is a true
mica-slate, identical in mineral character (as it is also in dip and
direction) with that on Loch Hope and the Kyle of Tongue.
On the other hand, rocks quite as hornblendic and as thoroughly
granitic in character are common in the eastern gneiss-district.
Such rocks may be seen near Strath Naver, Strathie Point, and on
the borders of Caithness in Sutherland; at Auch-na-Sheen and Loch
Carron in Ross-shire, and at Glen Elg and Isle Oronsay in Skye in
Inverness. Further east, in Banff-, Aberdeen-, and Kincardine-
shires, they are perhaps the more common varieties. In truth,
this peculiar character of the rock has no relation whatever to its
age or locality, but only, it would appear, to its proximity to the
* “Geog. of Sutherland,” Trans. of Highland Society, vol. xiii. (1889) p. 101.
t Ib. p. 78.

t Nicol, “ Quartzites of N.W. Scotland,” Quart. Journ. Geol. Soe. vol. xiii.
(1857) p. 24. § Zh. p. 28.

112 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 5,

great foci of igneous action. Wherever we find granitic and sy-
enitic eruptions, there the gneiss appears in these more coarsely
crystalline and hornblendic forms. Any person who examines the
western gneiss carefully will find these varieties prevailing only in
places where intrusive granite and syenite rocks abound, as, for
instance, near Scourie and Loch Inver, in parts of Lewis and
Harris, and on Loch Greinord. And it is these intrusive igneous
rocks, or rather the interior masses, of which these veins are the
mere external indications, which have expanded, and tilted up the
western gneiss, and thus produced that line of fault and compres-
sion which I have pointed out in the sections above described. So
far, therefore, from furnishing any objection to the theory main-
tained in this paper, the fact that the western gneiss has been thus
powerfully interlaced, swollen out, and modified, by veins and beds
of red granite, syenite, and other hornblende-rocks, by furnishing
a veritable and sufficient cause for the fracture and disturbance ob-
served along the line of junction, adds one more proof of its truth.

It is often assumed that the fine-grained gneiss, mica-slate, and
clay-slate are younger than the coarse-grained gneiss and horn-
blende-rocks; but on what grounds I have nowhere seen stated. In
the Southern Grampians I have shown that the very reverse relation
prevails, and that the clay-slates and mica-slates may be seen
troughing the central gneiss both on the south-east and north-
west. We see this along the great line of fracture intersecting the
primary formations, from the Murray Firth to the Linnhe Loch, and
still more on the southern margin of the Grampians. This remark-
able line of fracture, dividing the Old Red Sandstone from the pri-
mary formations, is the exact counterpart of the great line of fracture
now shown to exist in the north-west. As in the south, we find it
bringing up fine-grained gneiss, mica- or tale-slate, and even clay-
slate, succeeded further to the east by coarse-grained and hornblendic
gneiss.

Conclusion.

Before concluding, I must state that, even had it been proved that
the mica-slate or fine-grained gneiss of Sutherland truly overlaps
the quartzite, and that this overlap is the result of subsequent de-
position, the fact would not bear out the conclusions that have been
deduced from it, or establish that entire revolution in Scottish geology
which has been supposed. Proof would still be wanted that the
mica-slate of Loch Erriboll and Loch Hope is inferior to the great
masses of granitic gneiss in the centre of Sutherland. We might
ask for a continuous section through the interminable moors of the
Moin, and for evidence that the Kyle of Tongue and the huge syenite
domes of Ben Laoghal and Ben Stomino do not break the series and
bring up anew the lower and older gneiss. But such continuous
sections have never even been attempted, either there or through the
wilds of Assynt and Strath Oykill, still less across the mountain-
fastnesses of the Dirry Moor and Fannich Forest, so as to assure us
that no older underlying gneiss comes up there. ‘Till this is done,

1860. ] NICOL—N.W. HIGHLANDS. 113

there is no evidence to connect the great mass of crystalline schists
stretching from the north coast of Sutherland to the south of Inver-
ness-shire more closely with the mica-slates of Ben Hope than with
the gneiss of Scourie, Loch Inver, and the Gairloch, or to justify us
in throwing aside mineral characters for some assumed synchronism
in the age of the original, but now wholly altered, deposits.

No such revolution in Scottish geology is, however, required. The
sections, when carefully examined, are clear and simple, and quite
analogous to those of other mountain-regions. Every fact and section
alleged in proof of the recent origin of the eastern crystalline strata
appears on investigation to lead directly to the reverse conclusion.
At Durine, the mica-slate of the Bishop’s Castle, stated to overlie the
limestone, does not show a single calcareous bed in a thickness of
1000 to 2000 feet of strata; and the same mica-slates are forced
up from below the limestone, by igneous action, in the very centre
of the field. At Whiten Head and Loch Erriboll, the quartzites and
limestone, alleged to dip under the gneiss, are in part separated from
it by intrusive rocks, or meet it in wholly discordant position, often
so inverted and denuded that the upper limestone is entirely cut out
before reaching the line of supposed overlap. So too it is on Loch
More and Loch Glen Coul, where mere fragments of the quartzite
series are left abutting against, not dipping under, the old gneiss, or
separated from it by intrusive igneous rocks. In Assynt the so-
called “ upper quartz-rock” is proved to have no existence, but to
be a mere upturn of the old quartzite, which is seen resting on the
gneiss for miles along its N.E. margin, and on the 8.E. is divided
from it by a line of fault with huge intrusive masses of granite and
porphyry. Further south, in Cromarty- and Ross-shires, the same
phenomena prevail. The newer, overlying strata—whether the
limestone, the quartzite, or the Red Sandstone—always overlie or
abut against, never dip under, the older eastern gneiss. In Skye,
finally, the Red Sandstone, the oldest overlying deposit, dipping N.W.,
rests on the eastern gneiss dipping 8.E., and thus in an entirely
discordant position. Such are the facts and sections on which I
have no hesitation in asking a verdict in favour of the old, long-
established principles of Scottish geology.

VOL, XVYII.—PART I. i

114

DONATIONS

TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From July 1st, 1860, to October 31st, 1860.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. Vol. xxx.
Nos. 88,89. July—Sept.1860. From Prof. Silliman, For. MGS.

T. Parsons.—Origin of Species, 1.

T. T. de Schubert’s ‘The true Figure of the Earth,’ noticed, 46,

L. Lesquereux.—Coal- formations of North America, 65.

H.. How.—Oil-coal of Pictou, Nova Scotia, and Coals, 74.

E. B. Andrews, E. W. Evans, D. W. Johnson, and J, L. Smith.—
Meteoric Stones, 105.

F. Antisell’s ‘The Manufacture of Photogenic or Hydro-carbon
Coals,’ noticed, 112. :

T. S. Hunt.—Some points in Chemical Geology, 153.

L. Agassiz.—Origin of Species, 142.

D. Kirkwood.—The Nebular Hypothesis, 161.

H. A. Newton.—Meteor of November 1859, 186.

J. P. Cooke.—Crystalline form and chemical composition, 194.

C. U. Shepard.—Several American Meteorites, 204. .

C. Darwin’s ‘ Origin of Species,’ noticed, 226.

F. H. Bradley. —New Trilobite from the Potsdam Sandstone, 241.

J. W. Mallet.—Artificial crystallization of Metallic Copper and
dinoxyd of Copper, 253.

Antisell’s ‘On Hydrocarbon-oils from Coal,’ noticed, 254.

J. S. Newberry.—Cretaceous (?) plants of North America, 273.

C. S. Lyman.—The Meteor of July 20, 1860, 293.

E. W. Evans.—The Meteor of May 1, 1860, 296.

E. C. Herrick.—Shooting Stars of August 9-10, 1860, 296.

Oil-wells of Pennsylvania and Ohio, 305.

T. E. Wormley.—Temperature of Artesian Well at Columbus, Ohio,
306.

Bengal Asiatic Society. Journal. New Series. No. 95 (1858,
No. 5). 1860.
Nos. 102, 103 (1860, Nos. 1, 2).

G. von Liebig.—Barren Island, 1 (plate).
H, L, Thuillier.—Survey of Kashmir , 20,

DONATIONS. ills

Berlin. Zeitschrift der Deutsch. geol. Gesellschaft, Band xi,
Heft 4. 1859.

Verhandlungen, 475; Briefliche Mittheilungen, 478,

C. Rammelsberg.—Ueber die mineralogische Zusammensetzung der
Vesuvlaven und das Vorkommen des Nephelins in denselben, 495,

F. Zirkel.—Die trachytischen Gesteine der Hifel, 507 (map).

F. Roemer.—Bericht tiber eine geologische Reise nach Norwegen im
Sommer 1859, 541.

L. Zeuschner.—Ueber die oberen eociinen Schichten in den Thalern
der Tatra und des Nirne-Tatry-Gebirges, 590.

Bordeaux. Actes de la Soc. Linnéenne de. 3 Sér. Vol. i. 1860.

L. Fossat.—Sur une Tortue fossile trouvée & Moissac, et sur les Ter-
___tiaires des environs de cette ville, 71.
Mairand.—Sur les dépéts littoraux observés de Nantes 4 Bordeaux,
76 (plate).
V. Raulin.—Description physique de Vile de Créte, 109, 307, 491.
A, Paquerée.—Excursion aux erottes d’Arcy-sur-Cure (Yonne), 470,

Boston. American Academy of Arts and Sciences. Proceedings,
vol.iv. Sheets 12-31.

A. Gray, L. Agassiz, A. A. Gould, and others.—The flora of Japan
and the United States, and on the Distribution of Plants in the
Northern temperate zone, 131, 171, 195, 201.

C. T. Jackson.—Analysis of Bornite from Georgia, 196.

Obituary notices of P. Cleaveland, R. Brown, A. von Humboldt
(by L. Agassiz), 226.

——. Society of Natural History. Proceedings, vol. vi. ‘Sheets
23-28.

L. Agassiz.—Coral-reefs of Florida, 364, 373,
Weinland,—Corals of Hayti, 364.

James Deane, Obituary Notice of, by T. T. Bouvé, 391.
T. T. Bouvé and C. 8. Hale.—Zeuglodon cetoides, 421.

Vol. vii. Sheets 1-9.

C. T. Jackson.—Gold and Iron-ore, 22.
—. Metamorphism, 30.
——. Silver and Copper of Lake Superior, 31.
eM Loans Recent Eruption of Mauna Loa, Sandwich Islands,
9 Otte
C. T. Jackson.—Thermal Springs, 45.
W. B. Rogers.—Increace of temperature at great depths, 47.
T. T. Bouvé.—-Fossil Footmarks of the Connecticut Valley, 49.
ae Rogers.—Tertiay Infusorial Earth of Virginia and Maryland,
W. P. Blake.—Mineral resources of the Rocky Mountain-chain, in-
cluding Gold-field, 64.
A. M. Edwa= is.—Infusorial Marl from Milwaukee, 79.
oe ‘ ackson and J. H. Blake.—Frozen Well at Brandon, Vermont,
, 155.
H. Bryant and W. B. Rogers.—Bahama Islands, 85.
W. B. Rogers,—Coal-bearing Rocks of Ma’re, 86.
C. T. Jackson.—Compact specular Iron-ore from Phillipsherg, New
Jersey, 136,
12

116 DONATIONS.

Breslau. Sieben-und-dreissigster Jahres-Bericht der Schlesischen
Gesellschaft fiir vaterlindische Kultur. 1859.

Sadebeck.—Ueber die Vorberge des Eulengebirges, 17.

F, Roemer.—Ueber eine Sammlung von Zinkerzen, 18.

Ueber in Schlesien vorkommende Reste der Crustaceen-

Gattung Pterygotus, 19.

Erliuterung der Flotzkarte ées westphalischen Steinkohlen-

Gebirges, 19.

Ueber die allgemeine geognostischen und physikalischen
Verhaltnisse Norwegens, 19.

H. Goeppert.—Ueber das Vorkommen versteinter Holzer in Schlesien,

1

——. Ueber eine Zusammenstellung der Beobachtungen iiber ver-
steinte Walder, 25.
Brussels. Annuaire de l’Académie Royale de Belgique. 1860.
Quetelet.—Obituary notice of Humboldt, 97.

Bulletins de l’Acad. Roy. de Belgique. 28* Année, 2m™é¢
Ser. Vol. vu. 1859.

G. Dewalque.—Sur le fer oxydé octaédrique dans le grés de Lux-
embourg, 412.
Vol. vi. 1859.

Van Raemdouck.—Sur une découverte d’ossements fossiles faite &
Saint-Nicolas, 107, 109, 123, 197.

. Mémoires couronnés et autres Mémoires publiés par l Acad.
Roy. de Belgique. Collection in 8vo. Vol. ix. 1859.

Caen. Mémoires de la Soc. Linn, de Normandie. Années 1856-
57-58-59. Vol. xi. 1860,

E. Deslongchamps.—Sur les Plicatules fossiles des Terrains du Cal-
vados, et sur quelques autres genres voisins ou démembrés de ces
coquilles, 1 (14 plates).

E. de Fromentel.—Introduction 4 l’étude des éponges fossiles, 165

G plates).

E. E. Deslongchamps.—Sur les Brachiopodes du Kelloway-Rock ou
Zone ferrugineuse du Terrain Callovien dans le Nord-ouest de la
France, 251 (6 plates).

Cambridge, U.S. American Academy, Memoirs. New Series.
Vol. vi. Part 2: 1859.

Canadian Journal. New Series. Nos. 28, 29. July—Sept. 1860.

E, J. Chapman.—New species of Agelacrinites, 358 (figure).

C. Darwin's ‘On the Origin of Species,’ noticed, 367.

J. H. Dumble.—Contraction and expansion of Ice, 418.

T. 8. Hunt.—Intrusive rocks of Montreal, 426.

i. J. Chapman.—Geology of Hastings County, Canada West, 470.
—. Crystals of Idocrase, 474.

—. New Blowpipe-support, 474.

DONATIONS. 117

Canadian Naturalist and Geologist, and Proceedings of the Natural
History Society of Montreal. Vol.v, Nos.3,4. June-August,
1860.

E. Billings.—New Lower Silurian Fossils front Canada, 161 (figures).

J. W. Dawson.—Tertiary Fossils from Labrador, Maine, &e., 188.

——. Fossils from the Coal of Nova Scotia, 222.

W. E. Logan. Fossil Track of an animal in the Potsdam sandstone,
279 (figures).

H. Poole.—Coal-fields of Pictou, 285.

D. Honeyman.—Fossiliferous Silurian rocks in Eastern Nova Scotia,
293.

E. Billings.—New species of Fossils from the Limestone near Quebec,
301 (figures).

J.S. Newberry.—The oil-wells of Mecca, Ohio, 325.

Chemical Society. Quarterly Journal. Nos. 50, 51 (Vol. xiii.
Nos. 2,3). July-October. 1860.

G. H. Makins.—Loss of precious Metal in Assaying, 97.
C. E. Long.—Crystallized Sodium and Potassium, 122. |
L. Playfair.—Baudrimont’s Protosulphide of Carbon, 268.

Cherbourg, Mémoires de la Soc. Imp. des Se. Nat. de. Vol. vi.
1858. 1859.

Bonissent.—Sur le département de la Manche, 73.
J. Lesdos.—Sur un gisement de Sulfate de Baryte 4 Sideville, 372.
H. Jouan.—Sur les iles basses et les récifs de corail, 380.

Copenhagen. Oversigt over det Kel. danske Videnskabernes Sel-
skabs Forhandlinger, og dets Medlemmers Arbeider i Aaret 1859.

Boucher de Perthes.—Flintoldlager i Grusbakker ved Amiens, 125,
191.

Worsaae.—Jagttagelser til en ny Inddeling af den Steenalderen, 98.

Steenstrup.—Bemerkninger imod deune Tvedeling (Steenalderen),
IZA.

——. Questiones que in a. 1860 proponuntur a Soc. Reg. Danica
Scientiarum cum premii promissu.

Critic. Nos. 522-525, 533-538.

Meetings of Scientific Societies, &e.

Meeting of the British Association, 28, 51, 78.

D. T. Ansted’s ‘Geological Gossip,’ noticed, 107.

A. C. Ramsay’s ‘The Old Glaciers of Switzerland and North Wales,’
noticed, 107.

T. Tyndall’s ‘The Glaciers of the Alps,’ noticed, 188.

Edinburgh Royal Physical Society. Proceedings. 1854-58. Vol. i.
1858.

M. F. Heddle.—Oxalates in .the Mineral Kingdom; Analyses of
Conistonite and Heddlite, 4.

A. Geikie,—Liassie Fossils from Pabba and Skye, 6.

A. Bryson.— Worm-tracks in Silurian Slates, 7.

——. _Diatoms in the Silurian Slates of Scotland, 9.

M. F. Heddle.—Analysis of Datholite from Glen Farey, 9.

H. Miller.—Effects of frost on Marine Molluscs, 11.

118 DONATIONS,

Edinburgh Royal Physical Society (continued).

C. W. Peach.—Bryozoa, &c. in the Boulder-clay of Caithness, 18.

——. Fossils from the Limestones of Durness, 23.

M. F. Heddle.—Galactite of Haidinger ; Analysis of Scottish Natro-
lites, 51.

——. Mesolite, Fardelite (Mesole), and Antrimolite, 55.

D. Page.— Woodocrinus macrodactylus, and new fossil Crustaceans,
55, 56.

M. F. Heddle.—Uigite, 57.

J. M‘Farlane.—Shells and Reindeer’s horn found at Croftamie in
Dumbartonshire, 163, 218 (figures).

J. A. Smith.—Seales of Holoptychius from Roxburghshire, 168.

A. Taylor. —Contemporaneity in age of the “fountain” and the
“ Burdiehouse”’ Limestone of Linlithgows hire, 244,

A. Bryson.—Apophyllite at Ratho, 245.

C. W: Peach.—Diatomaceous Marls near Wick, 245.

W. Wood.—Geology of Elie, 250.

A. Dalyell. —Analys ses of three Waters from Palestine, 251.

J. Fleming.—Chalk-flints near Leith, 262.

J. MBain.—T wo Fossils found in Shale below St. Anthony’s Chapel,
Arthur’s Seat, 267.

Skull of a Wombat from the Bone-caves of Australia, with
remarks on the Marsupiata, 373.

A. Rose.—Heematite on the Garpel, Ayrshire, 378.

A. Taylor.—An Artesian Spring near Wester Whitburn, Linlith-
gowshire, 396.

W. Oliphant.—Lienite from Ballaarat, Australia, 405,

C. W. Peach.—Beekite and oolitic quartz at Durness, 429.

W. Rhind.—Coal found in a slate-quarry in the Island of Seil, 439.

G. Forrest and J. A. Smith.—Granite in Midlothian, 463.

W. Carruthers.—Graptolites of Dumfriesshire, including thres new
species, 466 (figures).

Ethnological Society. Report of Council, May 30, 1860.

Geologist. Vol. iii. Nos.31-34, July—Oct. 1860.

S. J. Mackie.—Geology of the Sea, 241.

W. S. Horton.—Stonesfield Slate, 249.

T. Dayvidson.—Carboniferous Brachiopods of Scotland, 258.

Proceedings of Societies, 270, 298, 379.

Notes and Queries, 271, 317, 547, 577.

G. V. Dunoyer.—Vertical Veins of Limestone in Slate at Temple-
more, 272.

H. Mitchell.—New Fossils from the Lower Old Red Sandstone of
Scotland, 275.

Reviews, O77,

8. J. Mackie.—Geology of Folkestone, 281, 321, 350.

E, Suess.—Distribution of the Brachiopoda, 235,

J. W. Kirkby.—Sandpipes in the Magnesian Limestone of Durham,
293, 329.

Lord W rottesley.—Address to the British Association, 298.

E. Hull.—The Blenheim Iron-ore and the Oolite at Stonesfield, 303.

H. B. Tristram.—Geology of the Sahara of Algeria, 505.

J. F. Whiteaves.—Invertebrate fauna of the Lower Oolites of Oxford-
shire, 307.

W. Lister.—Fossil Reptilian Footprints in the New Red Sandstone
near Wolverhampton, 308.

DONATIONS. 119

Geologist (continued).

W. Pengelly.—Devonian Fossils of Devon and Cornwall, 309.

T. Wright.—Avicula contorta beds and. Lower Lias, 310.

R. Harkness.—Metamorphic rocks of the North of Ireland, 311,

F. Anca de Mangalviti—T wo ossiferous Caves in Sicily, 312.

W. 8. Symonds.—Geological habitats of some of the rarer British
Plants, 315.

J. Dingle.—Corrugation of Strata near Mountains, 314.

J. A. Knipe.—Tynedale Coalfield and Whinsill, 315.

C. Moone.—Three cubic yards of Triassic Harth and its contents, 315.

S. P. Woodward.—An Ammonite with the Operculum in place, 328.

W. Powrie.—Old Red Sandstone and its Fossil Fish in Forfarshire,
336,

T. R. Jones.—Tertiary Ironsand of the North Downs, 339.

G. D. Gibb.—Canadian Caverns, 341 (8 plates).

H. C. Hodge.—Ossiferous Caverns at Oreston, 343, 377.

S. J. Mackie.—First Traces of Man on the Earth, 370.

J. J. W. Watson.—Metalliferous saddles in the Lower Carboniferous
rocks of Derbyshire and N. Staffordshire, 357.

Giessen. Achter Bericht der oberhessischen Gesellschaft fiir Natur-
und Heilkunde. 1860.

H. Hoffmann.—Vereleichende Studien zur Lehre von der Boden-~
stetigkeit der Pflanzen, | (map).

O. Volger.—Thatsachen zur Beurtheilung alterer und neuerer geo-
logischer Anschauungsweisen, 13.

C. H. G. yon Heiden.—Fossile Gallen auf Blattern aus den Braun-
kohlengruben yon Salzhausen, 63.

Seibert.—Zur Geologie des Odenwaldes, 76.

O. Buchner.—Ueber Feuermeteore und Meteoriten, 82.

Halle. Zeitschrift fiir die gesammten Naturwissenschaften, heraus-
gegeben von dem Naturw. Vereine ftir Sachsen u. Thiiringen in
Halle, redigirt von C. Giebel und W. Heintz. Jahrgang 1859.
Vole aii 1859!

W. Heintz.—Ueber den Stasfurtit, 1.

—. Ueber die Zusammensetzung des Boracits, 105.

LL. Witte.—Ueber die Vertheilung der Wirme auf der Erdober-
flache, 11.

F, Ulrich.—Uehber das Zechsteingebirge zwischen Osterode und
Badenhausen am 8.-W. Harzrande, 189 (plate).

E. Séchting.—Feldspathlaystalle im Quarz, 199, 452.

R. Dieck und W. Heintz.—Analyse des Aluminits von Presslers Berg
bei Halle, 265, 368.

Th. Liebe.—Ueber die bisherigen Resultate des Geraer Bohrver-
suches, 322.

i den Hinschluss von Fliissigkeiten in Mineralien,

Notices of works on Geology, Mineralogy, Paleontology, &e.

—. ——. Jahrgang 1859. Vol. xiv. 1859.

J. A. Hjalmarson.—Ueber die Insel St. Domingo, 12.
A. W. Stiehler.—Zu Pleuromeia aus dem Buntsandsteine bei Bern-
burg, 190.

120 DONATIONS.

Halle. Zeitschrift fir die gesammten Naturwissenschaften. Vol.
XIV. (continued).

R. Eisel.—Zur Umgebung von Gera; iiber dasige Dolomite als
Aequivalente des Kupferschiefers, 345.

W. Heintz.—Ueber den Stasfurtit, 351.

R. Richter.—Zur Petrographie des Thiivinger Waldes, 352.

J. Hecker.—lirfahrungen uber das Vorkommen der Sanderze in den
sangerhauser und mansfeldischen Revieren, 445 (2 plates).

C. Giebel.—F ora des siichsisch-thiiringischen Braunkohlenbeckens,
485,

Notices of works on Geology, Mineralogy, Paleontology, &e.

Heidelberg. Verhandlungen des naturhistorisch-medizinischen Ver-
eins. Vol.i. No. 2.

Horticultural Society of London. Proceedings. Vol. i. Nos. 14-17.
July—October, 1860.

International Statistical Congress. Programme of the Fourth Ses-
sion. 1860.

R. Hunt.—Statistics of Mineral Produce, &c., 85.

Leeds Philosophical and Literary Society. Annual Report for
1859-60. 1860.

Liége. Mémoires de la Soc. Roy. des Sciences. Vol. xv. 1860.

Linnean Society. Journal of the Proceedings. July 18. Supple-
mental to Vol. iv. Zoology.

Literary Gazette. New Series. Vol. v. Nos. 106-122. July—
Oct. 1860.
Meetings of Scientific Societies, &e.
Meeting of the British Association, 807.
Meeting of the International Statistical Congress, 16, 41.
J. Tyndall’s ‘The Glaciers of the Alps,’ noticed, 27.
Earthquake in Kent, 251.

Liverpool Literary and Philosophical Society. Proceedings. No. 14.

1859-60. 1860.
G. H. Morton.—Traces of Icebergs near Liverpool, 55.

Basement-bed of the Keuper in Wirral and the 8. W. of Lan-
cashire, 148.

C. Collingwood.—Homomorphism or Organic Representative Form,
181.

T. Dobson.—Explosions in Coal-mines, 217.

H. H. Higeins—Stony Corals, 230 (figures).

. London, Edinburgh, and Dublin Philosophical Magazine. 4th
Series. Vol. xx. Nos. 130-183. Juiy—Oct. 1860. From
Dr. W. Francis, F.GS.

J. Pilbrow.—Well-section near Gosport, 84.

J. Prestwich.—London Clay in Norfolk, 84.

T. R. Jones and W. K. Parker.—Fossil Foraminifera from Chel-

laston, 85,

DONATIONS. 121

London, Edinburgh, and Dublin Philosophical Magazine (continued).

W.S. Symonds.—Reptiliterous Sandstones of Elgin, 85.

Anca.—Bone-caves in Northern Sicily, 86.

A. H. Church and 1. Owen.—Destructive distillation of Peat, 110.

Breithaupt.—Thirteen systems of Crystallization and their optical
characters, 129.

G. P. Wall.—Geology of Venezuela and Trinidad, 164.

C. Sainte-Claire Deville.—Silicic Acid, 175.

J. H. Pratt.—Thickness of the Earth’s Crust, 194.

F. C. Calvert and G. C. Lowe.—Expansion of Metals and Alloys, 230.

HE. Lartet.—Coexistence of Man with certain extinct quadrupeds, 239.

W. P. Jervis.—Miocene rocks and minerals of Tuscany, 240.

H. Falconer.—Bone-caves of Gower, South Wales, 241.

D. Campbell.—Arsenic and Antimony in Streams and Rivers, 304.

Longman’s Monthly List. Nos. 211, 214. July, Oct. 1860.

Mechanics’ Magazine. NewSeries. Vol. ui. Nos. 80-96. July-
Oct. 1860.
Meetings of Scientific Societies, &c.
J. A. Davies.—Molecular alteration in stone, metal, wood, &c., 265.

Melbourne. Mining Surveyors’ Reports: furnished by the Mining
Surveyors of Victoria to the Board of Science. Nos. 9-15.
January—July, 1860.

Milan. Atti del R. Istituto Lombardo di Scienze, Lettere ed Arti.
Vol.i. Fasc. xvii.—xx. 1860.

Mining Review. Vol. iii. Nos. 89-95, 99, 103.

Notices of Scientific Meetings, &c.

Munich. Abhandlungen der math.-phys. Classe der konigl. bayer.
Akad. d. Wissensch. Vol. vii. Parts 1&2. 1857-58.

A. Vogel und G. C. Reischauer.—Ueber Bleysesquiphosphat, 1.

A. Wagner.—Neue Beitrage zur Kenntniss der fossilen Saugethier-
Ueberreste von Pikermi, 109 (7 plates).

C. F. Schoenbein.—Ueber metallische Superoxyde, 159.

A. Wagner.—Neue Beitrage zur Kenntniss der urweltlichen Fauna
des lithographischen Schiefers (Saurier), 413 (6 plates).

—. Almanach d.k. bayer. Akad. d. Wiss. f. das Jahr 1859.

Magnetische Ortsbestimmungen an verschiedenen Puncten
des Konigreichs Bayern und an einigen auswirtigen Stationen.
I. und II. Theil. 1854-56. 8vo.

New Zealand Examiner. No.6. June 13, 1860.

Offenbach. Erster Bericht des offenbacher Vereins fir Natur-
kunde uber seine Thiatigkeit yon seiner Grindung am 10. Marz
1859, bis zum 13. Mai 1860. 1860.

O. Volger.— Teleosteus primevus, Volger. Erste Spur eines Grathen-

fisches im Uebergangsgebirge aus dem rheinischen Dachschiefer
yon Caub, 37 (plate).

122 DONATIONS.

Paris. Annuaire de l'Institut des Provinces, des Sociétés savantes —
et des Congres scientifiques. 2° Sér. Vol. ii. 1860.

G. Cotteau. Rapport sur les progrés de la Géologie en France pen-
dant année 1858, 54.

Ecole des Mines; Annales des Mines. 5° Sér. Vol. xvi.
5° Livr. et 6¢ Livr. de 1859. 1859.

Daubrée.—Sur le metamorphisme et sur la formation des roches
cristallines 155, 393.

Descloizeaux.—Sur les formes cristallines et les propriétés optiques
de la zoisite, de la sillimanite et de la vohlerite, et sur une nou-
velle disposition du microscope polarisant, 219.

Lebleu.—Lavage de la houille aux mines de houille de Brassac
(Puy-de-Dome et Haute Loire), 243.

Delesse.—Sur les pseudomorphoses, 517,

Julien.—Sur la métallurgie du zine dans la haute Silésie, 477.

Sur l'industrie minérale dans le Wurtemberg, 531.

Sur une huile minérale recueillie a la surface du sol sur les bords de
la riviére Alleghany, 541.

Sur la production métallique du Chili, 545.

De la production des métaux dans la Grande-Bretagne en 1858, et
dans quelques autres contrées, 546.

Sur les changements de température produits par l’approfondisse-
ment et par l’extension des mines, 571.

Sur les gisements auriféres et platiniféres de ’Oregon, 573.

Sur les gisements auriféres de Nouvelle-Galles (Australie), 577.

Vol. xvu. J1¢ Livr. de 1860. 1860.

L. Moissenet.—Extraits des travaux du bureau d’essai (année
1859), 1.

‘Extraits de chimie (travaux de 1859), 19.

Tournaire.—Les travaux du laboratoire de chimie de Clermont-
Ferraud de 1856-59, 35.

Senarmont, de.—Extraits de minéralogie, 69.

Marsilly, de C. de—Les houilléres du Nord et du Pas-de-Calais,

107.
Comptes Rendus des Séances de VAcad. des Sc. 1860.

Prem. Semestre. Vol. 1. Nos. 19-26.

eS =. «Dei. sent. Vol. tee NO@s a=.

a) = Dables) Mens, seme tong. sav ol sein:

Damour et Leymerie.—Sur l’aérolithe de Montrejeau, 31, 247.

Debray.—Sur la reproduction artificielle de ’Azurite, 218.

D’Archiac.—Rapport sur un Mémoire de M. A. Gaudry intitulé
“Géologie de Vile de Ce 229, :

E. de Beaumont.—Sur une Carte géologique du Dauphiné par M. Ch.
Lary, 185.

Vezian.—Sur un systéme stratigraphique perpendiculaire au systéme
des Alpes occidentales, et du méme age, 202. igs x

Secchi.—Le tremblement de terre de Norcia ressenti jusqu’a Rome,
346.

H. Ste.-Claire Deville——Sur un nouveau minerai de vanadium, 210.

P. Beauvallet.—Sur la présence du vanadium dans V’argile de Gen-
tilly, 301. ? By

Domeyko.—Sur divers fossiles et minéraux envoyés du Chili, 539.

DONATIONS. 123

Paris. Comptes Rendus (continued).

A. Gaudry.—Os de cheval et de boeuf d’espéces perdues trouvés avec
des haches de piérre dans une méme couche de diluvium, 453, 465.

G. Pouchet.—Sur un instrument en silex trouvé par lui dans le ter-
rain de transport de St.-Acheul, 501.

Boucher de Perthes.—Sur les silex taillés des bancs diluviens de la
Somme, 581.

J. Prestwich.—Sur la découverte d’instruments en silex associés &
des restes de mammiféres d’espéces perdues, 634, 859.

D’Orbigny.—Sur le diluvium & coquilles lacustres de Joinville-le-
Pont, 791.

Leymerie.—Effets du mouvement primitif des grands courants d’eau
aux époques antérieures & la nétre, 795.

K. de Fourcy.—Carte géologique du Loiret, 941.
Radiguel.—Sur des restes trés-anciens de l'industrie humaine trouvés
dans le terrain de transport des environs de Paris, 677, 756, 988,
Chazereau.—Sur des haches en silex trouvées dans le département
du Loiret, 1013.

Gervais.—Sur une espéce de porc-épic fossile des bréches osseuses
de Vile de Ratoneau, 511.

Jackson.—Sur Videntité du Paradoxides Harlani et du P. Terre-
nove, 859.

Sur quelques observations faites & Vile de Terre-Neuve et en
Californie, &c., 46.

Moissenet.—Couches trayersées dans un puits foré a Louisville
(Kentucky), 517.

Meugy.—Sur l’origine de certains filons, 520.

De Luca.—Recherches chimiques sur le calcaire d’Avane en Toscane,
308.

A. Sismonda.—Sur le calcaire fossilifére du fort de l’Hsseillon en
Maurienne, 410.

Delesse.—Etudes sur le métamorphisme, 467.

Fargeaud.—De l’influence du temps sur les actions chimiques, et des
changements qui peuvent en résulter dans certains fossiles, 558.

C. D’Orbigny et Hébert.—Sur Vage des poudingues de Nemours et
des sables coquilliers d’Armoy, 670, 848.

M. de Serres.—Sur les bréches osseuses de Vile de Ratoneau, 678.

Altérations des os observées chez des vertébrés de l’ancien

monde, 95.

De Vextinction du plusieurs espéces animales depuis Vappa-

rition de Vhomme, 860.

De la classification des métaux d’aprés Haiiy, 738.

Fournet.—Sur l’oxyde de chrome de Faymont, 600.

Bebinet et Touche.—Influence du mouvement de rotation de la terre
sur les cours des riviéres, 638, 737,

Terreil.—Minerais de zinc sous forme oolithique, 553.

I. Desnoyers.—Pas d’animaux dans le gypse des environs de Paris,

Philadelphia Academy of Natural Sciences. Proceedings for 1860,
pp. 81-284.

W. M. Gabb.—New species of Cretaceous Fossils from New Jersey,
93 (plate).

T. 5. Hunt, Lesley, and Foulke.—Chemical Geology, 96.

Lesley.—Boulders of gneiss in State of New York, 97.

W. B. Rogers.—Alhertite or Albert-coal of New Brunswick, 98.

124 DONATIONS.

Philadelphia Academy of Natural Sciences (continued).
F. B. Meek and H. Engelmann.—Geology of “the Great Basin”
between the Wahsatch Mountains and the Sierra Nevada, 126.
R. E. Rogers.—Petroleum-wells of Ohio, 147.
I. B. Meek and F. V. Hayden.—Tertiary, Cretaceous, Jurassic, and
Permian Fossils from Nebraska, 175.
W. M. Gabb.—New species of Cretaceous Fossils from South Ame-
rica, 197 (plate).
H. C. Wood.—Carboniferous Flora of the United States, 236 (2
plates).
American Philosophical Society. Transactions. New Series.
Vola Part) 20 850"
F, V. Hayden.—Geological Sketch of the Estuary and Freshwater
Deposit of the Bad Lands of the J udith, 125 (map).
J. Leidy.—Extinct Vertebrata from the Judith River and Great
Lignite Formations of Nebraska, 139 (3 plates).
: . Proceedings. Vol. vi. Nos. 59, 60. June—Dec.
1858. Vol. vu. No. 61. January—June, 1859.
Trego and R. E. Rogers.—Mineral deposit from the Hot Springs of
Munnikwrun, on the Himalayas, 4.
J. Leidy.—Geology and Fossils of the Bad Lands of the Judith, 10.
Photographic Society. Journal. Nos. 99-102. July—Oct. 1860.

Quarterly Journal of Microscopical Science. No. 32,33. July and
October, 1860.
A. Kolliker.—Vegetable Parasites in the hard tissues of the Lower
Animals, 171 (plate).
Royal Asiatic Society of Great Britain and Ireland. Journal.
Vol. xviii. PartI. 1860.
Royal Astronomical Society. Memoirs. Vol. xxvii. 1860.
Royal College of Surgeons of England. Catalogue of the Museum.
Part I. Plants and Invertebrate Animals in the dried state. 1860.
Royal College of Surgeons of England. Observations and Reflections
on Geology, by John Hunter, F.R.S. Intended to serve as an
Introduction to the Catalogue of his Collection of Extraneous
Fossils. 1859.
Royal Geographical Society. Proceedings. Vol. iv. No. 4.
Earl de Grey and Ripon.—Anniversary Address.
Royal Society. Proceedings. Vol. x. Nos. 39, 40.
M. Faraday.—Regelation, 440.
E. W. Brayley.—Regelation in Water, Glass, &c., 450.
W. B. Carpenter.—Researches on Foraminifera, 506.
Obituary notices of R. Bright, W. J. Broderip, 1. K. Brunel, T.
Horsfield, G. T. Staunton, R. Stephenson, F. H. A. von Humboldt,
and others, i.—xliii.
St. Louis. Academy of Science. Transactions. Vol.i. No. 3.1859.
G. G. Shumard.—Geology of the Jornada del Muerto, New Mexico,
341.
B. F. Shumard.—Fossils from the Permian Strata of Texas and New
Mexico, 387 (plate).

DONATIONS. 125

St. Petersburg. Acad. Imp. des Sciences. Mémoires, 7° Série.
Vol.u. Nos. 1-3. 1859.

Bulletin. Vol. i. Nos. 4-9. 1860.

H. Abich.—Rapport sur ses occupations au Caucase, &c., 209, 364,
449,

N. Kokcharof.—Sur le Rutil et Paralogit, 229.

G. de Helmersen.—Description de quelques masses de cuivre natif,
521 (plate).

Ph. Brunn.—Le littoral de la Mer Noire entre le Dniépre et le
Dniéstre, d’aprés les cartes hydrographiques du XIV° et du XV°*
siécles, 573.

H. Goeppert.—Sur la Flore paléozoique inférieure, 414.

H. Struve.—Sur la présence du phosphore dans le fer de fonte et sur
quelques phosphures métalliques, 453.

J. F. Brandt et G. de Helmersen.—Recherches paléontologiques dans
la Russie méridionale, 553.

A. de Middendorffi—Les découvertes de grands mammiféres gelés
en Sibérie, 557.

Society of Arts. Journal. Nos. 398-414. July—Oct. 1860.

W. P. Jervis.—Mineral Resources of Tuscany, 689, 699, 728, 748,

755.
Stuttgart. Wiurttembergische naturw. Jahreshefte. 16. Jahrg.
Zweites und drittes Heft. 1860.

H. y. Fehling.—Chemische Untersuchung der Teinacher Mineral-
quellen, 129.

E. v. Martens.—Die classischen Conchylien-Namen, 175.

C. Baur.—Die Lagerungsverhiiltnisse des Lias auf dem linken Neckar-
Ufer, 265 (plate).

H. v. Fehling.—Steinsalz aus dem Schacht bei Friedrichshall, 292.

Tyneside Naturalists’ Field-club. Transactions. Vol.iv. Part 3.
1860.

H. B. Tristram.—Presidential Address, 191.

Vienna. Denkschriften d. k. Akad. d. Wissensch. Math.-nat.
Classe. Vol. xviii.

W. Haidinger und F. Menapace,—Eis der Donau, 1858, 1 (18 plates,
and tables).

—. Feierliche Sitzung der k. Akad. Wissensch. am 30. Mai
1859.

Jahrbuch d. k. k. geol. Reichsanstalt. 1860. xi. Jahrgang.
No.1. Janner—Miarz.

F, von Hauer.—Ueber die Verbreitung der Inzessdorfer- (Congerien-)
Schichten in Oesterreich, 1.

A. Kengott.—Der Hoernesit, ein neues Mineral aus dem Banat, 10.

K, M. Paul.—Hin geologisches Profil durch den Anniger bei Baden
im Randgebirge des Wiener Beckens, 12.

D. Stur.—Ueber die geologische Uebersichts-Aufnahme des Was-
sergebietes der Waag und Neutra, 17.

Verhandlungen, 1-99,

126 DONATIONS.

Vienna. Sitzungsberichte d.k. Akad. Wissensch. Math.-nat. Cl.
Vol. xxxix. Nos. 1-5. 1860. P

em ae Rutillaystalle von Graves’ Mount in Georgia,

S., 5.

V. von Zepharovich.—Ueber die Krystallformen des zweifach chrom-
sauren Ammoniak-Quecksilberchlorids, 17 (2 plates).

Hi. Suess.— Ueber die wohnsitze der Brachiopoden (2. Abschnitt), 151.

A. E. Reuss.—Die marinen Tertiirschichten Bohmens und ihre
Versteinerungen, 207 (8 plates).

A. Schrauf.—Krystallographisch-optische Untersuchungen iiber die
Identitiit des Wolnyn mit Schwerspath, 286 (8 plates).

K. von Hauer.—Ueber einige selensauren Salze und die Darstellung
der Selensiure, 299.

Ueber die Krystallisation und Darstellung einiger Verbin-
dungen, 438.

——. Ueber einige Verbindungen der Vanadinsiiure, 448.

W. Haidinger.—Ueber den Meteoreisenfall yon Hraschina bei
Agyram, 519.

K. von Hauer.—Krystallogenetische Beobachtungen, 611.

H. Dauber.—Ermittelung krystallographischer Constanten und des
Grades ihrer Zuverlissigkeit, 685 (5 plates).

Vol. xl. Nos. 7-12. 1860.

W. Haidinger.—Der Hoernesit, 18.

G. Tschermak.—Ueber Calcitkrystalle mit Kernen, 109 (plate).

. Ueber secundiire Mineralbildungen in dem Griinsteingebirge
bei Neutitschen, 113.

A. E. Reuss.—Die Foraminiferen der westphilischen Kreideforma-
tion, 147 (15 plates).

F. C. Schneider.—Ueber das chemische und elektrolytische Ver-
halten des Quecksilbers, 239.

E. Suess.—Ueber die Spuren eigenthiimlicher Eruptions-Erschei-
nungen am Dachstein-gebirge, 428.

W. Haidinger.—Eine Leitform der Meteoriten, 525 (2 plates).

K. yon Hauer.—Kvystallogenetische Beobachtungen, 539, 589 (8

lates).

¥ Btetdachnen Zit Kenntniss der fossilen Fischfauna Oester-

reichs, 555 (3 plates).

Warwickshire Naturalists’ and Archeologists’ Field-club. 1859.
Report.

———

Washington. Smithsonian Institution, Annual Report of the Board
of Regents of, for 1858. 1859.

Zoological Society of London. Proceedings. 1860. Parts 1 & 2.
January—June.

DONATIONS. 197

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. vi.
Nos. 31-34. July—October, 1860.

W. H. Baily.—New Pentacrinus from the Oxford Clay of Dorsetshire,
25, 152 (plate). :

—. New Solarium from the Upper Greensand of Dorsetshire, 28

late).

we Phakor and T. R. Jones—Nomenclature of the Foraminifera.
The Lamarckian Species, 29.

De Koninck, L.—Two new Species of Chiton from the Wenlock
Limestone, 91 (plate).

J. G. Jeftreys.—Origin of Species, 152. ‘

E. J. Chapman.—New species of Agelacrinites, and on the relations
of the genus, 157.

J. W. Dawson’s ‘ Archaia,’ noticed, 205.

W. B. Carpenter.—Foraminifera, 208.

L. Agassiz.—Origin of Species, 219.

H. Falconer.—Bone-caves of South Wales, 297.

Edinburgh New Philosophical Journal. New Series. No. 23, 24.
Vol. xii. No. 1, 2. July and October, 1860.

R. Edmonds.—Extraordinary Agitations of the Sea and Earthquakes
in the West of England in 1858-59, 1.

H. How.—Oil-coal of Pictou, Nova Scotia, 80.

W. S. Symonds.—Reptiliferous Sandstone of Elgin, 95.

T. Brown.—Lower Carboniferous rocks of the Fifeshire Coast, 115.

A. Geikie.—Chronology of the Trap-rocks of Scotland, 117.

W. Thomson and — Everett.—Underground Temperatures, 183, 187.

W. Rhind.—Reptiliferous sandstones of Morayshire, 153.

C. W. Peach.—Chalk-flints of Stroma and Caithness, 154.

J. M‘Bain.—Fossil bird-bones from New Zealand, 155.

C. Daubeny.—Elevation-theory of Volcanos, 173.

R. Edmonds.—Earthquake-shocks and Whirlwind in Cornwall, 208.

J. Davy.—Colour of the Rhone, 213.

Hector.—Geology of part of British North America, 225 (plate).

L. Beale.—Permanence of Species, 253.

J. Tyndall’s ‘ Glaciers of the Alps,’ noticed, 249.

C. Daubeny, R. Owen, T. Huxley, and others.—Origin of Species, 272.

C. H. Hitchcock and J. 8. Newberry.—Coal-beds of Rhode Island,
&¢., 282.

J. D. Whitney.—Lead-bearing regions of the North-west, 284.

J. 5. Newhberry.—Petroleum-wells of the Mississippi Valley, 287.

Q. A. Gilmore.—Hydraulic Cement, 293.

J. 8. Newberry.—Fossil Floree of North America, 305.

J. W. Dawson.—Climate of Canada in the Pleistocene Period, 309.

J. W. Flower.—Flint Implement from Amiens, 311.

H. D. Rogers.—Fossil Flint Implements, 314.

J. Pr ah a Noe Flint Implements from the valley of the Somme,

Institut, ?. 1° Section. Sc. Math. Phys. et Nat. Nos. 1883-1395.

——. 2° Sect. Se. Hist. Arch. et Phil. Nos. 292, 293 Gn one).
April and May.
Notices of Scientific Meetings, &c.

128 DONATIONS.

Leonhard und Bronn’s Neues Jahrbuch f. Min. u.s. w. Jahrgang
1860. Drittes Heft.

A. Streng.—Die Quarz-fiihrenden Porphyre des Harzes. I. Die
orauen Porphyre, 257.

Hi. Credner.—Die Grenz-Gebilde zwischen dem Keuper und dem
Lias am Seeberg bei Gotha und in Norddeutschland wberhaupt,
293 (plate).

K. G. Zimmermann.—Die Tertiér-Versteinerungen am Brothener
Strande bei Travemiinde, 320.

Letters: Notices of Books, Minerals, Geology, and Fossils.

Paleeontographica (H. von Meyer). Vol.vii. Part 3. July, 1860.
H. von Meyer.—Frésche aus Tertiaér-Gebilden Deutschland’s, 1238
(7 plates).
—— (H. von Meyer). Vol. vii. Part +. July, 1860.
R. Ludwig.—Fossile Pflanzen aus der altesten Abtheilung der
rheinisch-wetterauer Tertiir-Formation, 105 (14 plates).
—— (H. von Meyer). Vol. vii. Part 5. August, 1860.
R. Ludwig.—Fossile Pflanzen der rheinisch-wetterauer Tertiar-
Formation, 137 (15 plates).
— (W. Dunker). Vol.ix. Part 1. August, 1860.

TF. A. Roemer.—Zur_ geologischen Kenntniss des nordwestlichen
Harzgebirges, 1 (12 plates).

III. GEOLOGICAL AND MISCELLANEOUS BOOKS. —

Names of Donors in [talies.

Address of H.R.H. the Prince Consort on opening the International
Statistical Congress. 1860. From the International Statistical
Congress.

Allport, S. On the discovery of some Fossil Remains near Bahia
in Sonth America. With Notices of the Fossils by Professor
J. Morris, Sir P. Egerton, and T. Rupert Jones, Esq. 1860.
From T. R. Jones, F.GS.

XQ = ia
Anca, F. Sur deux Nouvelles Grottes 4 ossements fossiles decou-
vertes en Sicile en 1859.
Barrande, J. Colonies dans le bassin Silurien de la Bohéme. 1860.
——. Troncature normale ou périodique de la coquille dans cer-
tains céphalopodes paléozoiques. 1860.
Bergh, A. An Essay on the causes of distant alternate periodic
Inundations over the low lands of each Hemisphere. 1860.
Boeck, C. Bemerkninger angaaende Graptolitherne. 1851. From

(=)

Mis Excell. Count Platten.

DONATIONS. 129

Catalogue of the Contents of the Museum of the Royal College of
Surgeons of England. Part I. Plants and Invertebrate Animals
in the Dried State. 1860. From the R. Coll. Surgeons.

Chambers, R. Tracings of the North of Europe. 1850.

Daubeny, C. On the Elevation Theory of Volcanoes, in reply to a
Paper of Mr. Poulett Scrope, read before the Geological Society
Feb. 2, 1859. 1860.

Davidson, T. A Monograph of the Carboniferous Brachiopoda of
Scotland. 1860.

Dawson, J. W. Notice of Tertiary Fossils from Labrador, Maine,
&e. 1860.

Delesse, A. Recherches sur les Pseudomorphoses. 1859.

Desnoyers, J. Sur des empreintes de pas d’animaux dans le Gypse
des environs de Paris et particulicrement de la vallée de Mont-
morency. 1859.

Doue, J. M. B. de. De la fréquence comparée des vents supérieurs
et inferieurs sous le climat du Puy en Velay. 1851.

Favre, A. Observations relatives 4 la note de M. Emile Benoit sur
les Terrains Tertiaires entre le Jura et les Alpes. 1860.

Forchhammer, G. Om Sovandets Bestanddele og deres Fordeling i
Havet. 1859.

Frreke, H. Observations upon Mr. Darwin’s recently published
work ‘On the Origin of Species by Means of Natural Selection.’
1860.

Gabb, W. M. Catalogue of the Invertebrate Fossils of the Creta-
ceous Formation of the United States. 1859.

Gaudin, C. T., et Carlo Strozzi. Contributions 4 la Flore Fossile
Italienne. 4¢me Mémoire. Travertins Toscans. 1860.,

; . Mémoire sur quelques gisements de feuilles fossiles de
la Toscane. 1858.

, et G. de Rumine. Coupe de V’axe anticlinal au-dessous de
Lausanne. Nouveau gisement de feuilles fossiles 4 Lavaux, par
C. T. Gaudin. 1860.

, et P, de Mandralisca. Contributions 4 la Flore Fossile Ita-
lienne. Cinquicme Mémoire. Tufs volcaniques de Lipari. 1860.

Gesselet, J. Mémoire sur les terrains primaires do la Belgique.
1860.

Grant, R. EZ. Syllabus of Four Lectures on Foraminiferous Ani-
malcules, Polypiferous Animals, Insects, and Reptiles. 1860.
VOL, XVII.—PART I. Kk

130 DONATIONS.

Hall, J., and J. D. Whitney. Report on the Geological Survey of

. the State of Iowa, embracing the results of Investigations made
during portions of years 1855, 1856 & 1857. Vol.i. Part 1
(Geology). 1888.

—. ——. Vol.i. Part 2 (Paleontology). 1858.

Haven, C. H. Views on the vine-growing resources of St. Louis
and adjacent counties of Missouri. 1858.

Mislop, S. On the Tertiary deposits associated with Trap-rock in
the East Indies, with Descriptions of the Fossil Shells: and with
Descriptions of the Fossil Insects by A. Murray, Esq., and a Note
on the Fossil Cypride by T. R. Jones, Esq. 1860.

Holmes, F.S. Post-pleiocene Fossils of South Carolina. Nos. 6-10.
1859.

Horbye, J.C. Fortsatte lagttagelser over de erratiske Pheenomener.
From His Excell. Count Platten.

Observations sur les phénoménes d’Erosion en Norvége.
1857. From His Excell. Count Platten.

Hunter, J. Observations and Reflections on Geology. 1859. From
the Roy. Coll. of Surgeons.

Jervis, W. P. Mineral Resources of Tuscany. No. II. 1860.

Jones, T. R., and W. K. Parker. On the Rhizopodal Fauna of the
Mediterranean compared with that of the Italian and other Ter-
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Kjerulf, T. Das Christiania-Silurbecken chemisch-geognostisch
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Laugel, A. Mémoire sur la géologie du département d’Eure-et-
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Liancourt, C. A. de G. An appeal to Senates of Universities, &c.,
against the present mode of Teaching French and other Lan-
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M‘Andrew, R. Note on the comparative size of Marine Mollusca
in various Latitudes of the European Seas. 1860.

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kommenden Erscheinungen. Deutsch bearbeitet von L. H. Jeit-
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Martius, C. F. P. v. Denkrede auf Alexander von Humboldt.
1860.

Mitchell, H. Notice of New Fossils from the Lower Old Red Sand-
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DONATIONS. 131

Murchison, R. I. Nouvelle classification des anciennes roches du
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Supplemental Observations on the Order of the Ancient
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and the North-east of Scotland. 1860.

On the Relations of the Gneiss, Red Sandstone, and Quartzite
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Second Report of the Geological Survey in Kentucky made
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THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

DxcEmBeR 19, 1860.

The Rey. William Liston, Bushbury Vicarage, Wolverhampton ;
the Rey. Alfred Deck, A.M., Royal Military College, Sandhurst ;
and Charles Rooke, Esq., Bellevue Cottage, Scarborough, were elected
Fellows.

The following communications were read :—

1. On the Structure of the Sourn-West Hicuianps of Scornann.
By T. F. Jamzeson, Esq.

(Communicated by Sir R. I. Murchison, V.P.G.S. &c.)

CoNTENTS.

. Introduction: general arrangement of the rocks of the district,

. The anticlinal axis, and character of the strata composing it.
Succession of the older rocks in Bute.

. The geology of Knapdale.

. The relations of the rocks of Jura, &c., to those described.

. The greenstones of Knapdale ; metamorphic action; metallic veins.
. Probable age of the rocks described.

NID OUR Cote

§ 1. Tue following paper is an attempt to throw some light upon
the relations of those rocks which figure in our geological maps as
the mica-schist, clay-slate, the chlorite-series, and quartz-rock of
the South-western Highlands, and the prolongations of which, ran-
ging N.E. through the middle of Scotland, form so conspicuous a fea-
ture in the geology of that country.

An examination of these rocks, as displayed in Bute and Argyle-
shire, has led me to believe that from the quartz-rock of Jura to
the border of the Old Red Sandstone we have a conformable series

VOL. XVII.—PARY I. I

134 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

of strata which, although closely linked together, may be classed
into three distinct groups, namely :—

1. A set of lower grits, of immense thickness.

2. A great mass of thin-bedded slates.

3. A set of upper grits, with intercalated seams of slate.

Beds of limestone* occur here and there sparingly in all the three
divisions, the thickest I have met with being situated deep down in
the lower grits. These limestones appear to attain their greatest
development in the western extension of the strata, thinning out to
the eastward. The siliceous grits also seem to become purer and
more devoid of green sediment as we trace them to the west. All
the members of the series, namely the upper grits, slates, and lower
grits, have a persistent strike from $.W. to N.E. (sometimes in Bute
approaching to due N. and8.), following one another in conformable
order ; and the three groups graduate into each other where they
meet, in such a way as to show that they belong to one continuous
succession of deposits; and not only so, but the materials of which
they are composed seem to have been derived from very similar
sources: beds of the lower grit are often undistinguishable in hand-
specimens, or even in mass, from those of the upper, being made up
chiefly of water-worn grains of quartz, many of which are of a pecu-
har semitransparent bluish tint.

I selected the region lying between Rothesay and the Sound of
Jura as likely to afford the best insight into the disposition of these
rocks, and devoted my attention to the districts of Bute, Cowal,
Knapdale, and the line of the Crinan Canal}. In order to render the
following pages more intelligible, it is necessary, before going further,
to mention that the outlines of the chlorite-series, as laid down in
the map of Macculloch, and also in the smaller one of Nicol, are
incorrect in some places to a considerable degree. For instance,
almost all South Knapdale is brought into the chlorite-series, whereas
the coast-section across the strike of the beds from Barmore to In-
verneil, being a distance of about six miles, shows no chlorite-slate,
but is almost all a highly siliceous grit, often forming indeed a true
quartz-rock. On both sides of Loch Fyne also, in the neighbourhood
of Otter Ferry, and apparently for some distance up and down the

* T ought to mention that I did not myself observe any mass of limestone
in the middle division, or great body of slates, although it occurs closely asso-
ciated with slate amongst the upper grits. See, however, Macculloch, ‘ Western
Tsles,’ vol. ii. p. 458, where he says that the limestone “ peculiarly accompanies ”
the clay-slate. And Col. Imrie, in the Edinburgh Philosophical Transactions,
yol. vi., describing the section along the N. Esk in Kincardineshire, mentions
a bed of limestone, 6 feet thick, amongst the slate, and another, 12 feet thick,
between two thin layers of black shale. See also an interesting short notice by
Prof. James D. Forbes on the geology of the parish of Fordoun, in the ‘Statistical
Account of Kincardineshire,’ where he mentions a bed of limestone occurring
in the midst of the slate, and quarried at a place called Clattering-brigs. Daniel
Sharpe seems to have found no limestone in the slate at Brig o’ Cally, Birnam,
Stratherne, and Aberfoyle, nor in the Loch Lomond section, these being the
points where he examined it: see his paper in the Quart. Journ. Geol. Soc.,
vol. viii. p. 126.

+ A geological sketch-map of the district has been deposited by the author
in the Society’s Library.

1860. ] JAMIESON—S.W. HIGHLANDS. 135

loch, the strata are also very
quartzose with no chlorite-
schist; and the thickest and
most persistent bed of lime-
stone, lying at the base of
this immense quartz-deposit,
and ranging from Otter by
Barmore to Western Loch
Tarbert, is omitted; while
the whole district of Knap-
dale and Crinan is traversed
by great ranges of green-
stone, of which no indication
is given. The reason, how-
ever, why Macculloch omit-
ted these greenstones will be
afterwards more particularly
referred to.

§ 2. The rocks of the di-
strict under consideration
seem to have been thrown
into agreat undulation, whose
anticlinal axis extends from
the north of Cantyre, through
Cowal, by the head of Loch
Ridun, on to Loch Eck, while
the axisof thesynclinaltrough
seems to lie nearly on the line
of Loch Swen. (See the
woodcut.)

Macculloch, in his work
on the Western Isles (vol. u.
p-288), had remarked that in
Cantyre the mica-schist on
the eastern shore dips to the
E., and on the other side to
the W.; and Sir Roderick
Murchison (Quart. Journ.
Geol. Soe. vol. vii. p. 169) had
noticed a fine anticlinal fold
at Loch Eck. These obser-
vations led me to expect that
I should find a similar phe-
nomenon somewhere near the
north end of Bute; and ac-
cordingly I went in search of
it, and found it, not in Bute
itself, but a little to the north
of that island, in a high ridge
near the Tighnabruich steam-

L2

S.E.

Rothesay.

Bute.
[represented as too thin in Bute].

a. Lower grits.

b. Slates

ay).

Loch

Diagram-section ilustrating the supposed disposition of the Rocks from Jura to Rothesay.
Fyne. Cowal

d. Old Red Sandstone (and trap-rock at Rothes
c. Upper grits (and greenstones in Knapdale).

136 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

boat-quay, in the Kyles of Bute. There in the brow of a large hill
called Ben Y-Happel, whose height is probably somewhere about
1500 feet, the folding over of the strata is distinctly seen; and from
its summit I could trace the same anticlinal axis ranging away for
along distance in a direction about N.33° EK. The lowermost strata
brought up in this anticlinal fold, as displayed here and at the north
end of Cantyre, where also I examined them, consist of hard rugged
masses, much wrinkled and contorted, composed chiefly of quartz and
mica—although felspar is also to be found, but forming in most places
only a small proportion of the rock. Portions would be correctly
termed gneiss, even in the strict definition of that term; other por-
tions are more of the nature of mica-schist, and some of quartz-
rock; while a greenish substance, probably chlorite, is often added
to the whole, giving its hue to the rock. The colour, however,
varies from pale greenish-grey to reddish-brown ; and I observed
small glancing octahedral crystals of iron-ore in various places, both
near the Kyles of Bute and in Cantyre. Notwithstanding the me-
tamorphic aspect of these lower rocks, their original arenaceous cha-
racter is in many parts still apparent,—thick beds, finely laminated,
containing the same water-worn particles of blue and grey quartz
as are found throughout the whole series of both upper and lower
grits, being met with in various places, enclosed amongst others in
which the lines of deposition are confused and obliterated. But the
pervading feature of the rocks all about this anticlinal axis 1s their
highly corrugated and contorted aspect, with numerous segregations
of quartz. This axis, I am inclined to think, will be found to run
through the country for a very long distance, passing probably by
the head of Loch Lomond on to the valley of the Tay, where I ob-
served it on the same line of strike, at Aberfeldy, in 1859. Similar
masses of hard rugged gneiss and mica-schist rise up there ina
gentle dome-shaped curve, and are seen on both sides of the river,
more especially in the rocky face of Weem Craig, throwing off heavy
micaceous strata to S.E. and N.W.

From this ridge of Ben Y-Happel, if we proceed (south-east-
ward) across the Kyles through Bute, we pass over a continuous
series of rocks, following each other in quite conformable succession,
and all dipping steadily to 8.E., until we come to the Old Red Sand-
stone in the neighbourhood of Rothesay. In no part of Bute,
neither on the east side nor on the west, where I followed the whole
line of coast to the north of Scalpsie Bay, nor in the interior, did I
meet with a reversed or N.W. dip. If again we turn our faces in
the opposite direction (to the N.W.), towards Loch Fyne, we pass
over a similar series, all conformable and dipping in like manner to
the N.W.

§ 3. Taking the Bute or south-eastern section first (which is a
very satisfactory one, as the rocks are disposed with great regularity,
without any quantity of disturbing masses of an eruptive nature),
it will be found that after leaving the neighbourhood of the anti-
clinal axis the strata become gradually less and less contorted, falling
into regular parallel beds as we proceed across them; the quantity of

1860. ] JAMIESON—S.W. HIGHLANDS. 137

mica also becomes less; and the great body of the rocks along the
very clear section of the west shore from Kilmichael to Kilda-
vannan Point, where the slates commence (a distance of about three
miles), is found to be highly silieeous, often almost wholly of quartz ;
they are in fact altered sandstones, varying in quality from fine grit
to coarse indurated sand with grains of the size of peas or beans,
in which the water-worn character still remains quite distinct ;
nothing, however, so coarse as to be termed a conglomerate oc-
curred. These siliceous beds vary in colour, but are for the most
part of a pale greenish-grey. Although no decided beds of slate are
met with along this part of the section, yet there are some nests and
patches of fine sediment, and even a few thin seams here and there,
precisely similar in quality to the material of the thick beds of slate
that follow. These slates commence, as I have said, at Kildavannan
Point on the west, and at Ardmaleish Point on the east shore of
Bute, there being frequent alternations of grit and slate where they
first make their appearance. Near the base of these slates at Kilda-
vannan Point I found some arenacous beds composed of exceedingly
fine yellowish-green sand, often parted by seams of white sand, all
laminated in the most delicate manner, and even showing indications
of false-bedding; they also alternate with coarser-grained layers
similar in quality to the underlying grits.

The great mass of slates that follow consists of finely laminated
sediments, generally of a greenish colour, but containing also many
seams of dark-blue roofing-slate: these blue slates are not exclu-
sively confined to any one part of the series, being found in every
portion of this division; but they are perhaps most frequent near the
base and top. Many alternations of dark-blue and green slate are
seen. Iam led to notice this the more as the late Daniel Sharpe,
in his paper on the Southern Border of the Highlands (Quart. Journ.
Geol. Soe. vol. vii. p. 127), had distinguished them into two sepa-
rate formations, which he termed the dark-blue and the chloritic or
green slates,—a distinction perhaps correctly descriptive of some
localities, but evidently not of general application. These thin-
bedded sediments form a zone across Bute, extending on the west
side from Kildavannan Point to a place called Mecknoch, a short
distance to the north of Ardscalpsie Point, and on the east side
from Ardmaleish Point to Rothesay Bay. They vary in quality from
the finest clay-slate to slaty flag and thin-bedded grit; and there
are even a few seams of coarse-grained grit, with grains of the size
of peas or beans. Intercalated seams of mica-slate are also met
with. The colour is various, from dark purplish-blue to pale green,
silvery-grey, and brown; but the prevailing hue is greenish, and
the rock is thinly laminated. They had been the finely comminuted
sediment, the silty mud and clay, of the old sea-bottom, the grits
being the sand and gravel. So far as I noticed, the lines of deposition
are almost always quite distinct, being seldom obscured by cleavage.

Covering these thin-bedded slates I found a thick mass of grit,
forming a rugged hilly ridge stretching from Ardscalpsie Point to
Barone Park near Rothesay, and of which Barone Hill attains a height

138 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

of 538 feet. These grits cover a space at least a mile broad in the
middle of the island ; and as they dip at high angles to the 8.K., they
must evidently be of considerable thickness. They are the uppermost
of the old rocks as displayed in Bute, being bordered by the Old Red
Sandstone to the south along the hollow of Loch Fadd and Loch
Quien to Scalpsie Bay. The actual meeting of the two formations,
however, is not seen, except for an insignificant space at Ardscalpsie
Point ; and a good deal of trap appears to oceur along the boundary.
These grits are not, I believe, the lower grits brought up by a
fault; for they follow the slates quite conformably, without, so far as
I observed, any trap coming up between them. They contain at
least one band of dark-blue slate, near their base, and also differ
somewhat from the lower grits in containing a greater prevalence of
coarse-grained gravelly layers. There may be some fault at the N.E.
base of Barone Hill, where the ridge suddenly termimates; for a
great trap-dyke crosses the island there in a N.W. direction, and,
traversing the slates, runs out to the shore a little to the south of
Ettrick Bay; but whether there actually is a fault I could not
determine, owing to the nature of the ground.

This Bute section, then, shows at its base a set of contorted micaceous
grits, followed by a great thickness of siliceous grit, above which
comes an extensive development of thin-bedded sediments or slates,
these slates being covered by a mass of grit containing at least one
seam of slate, and having more frequent beds of coarse gravelly tex-
ture than are met with im the lower grits. I observed no decided
bed of limestone in these old rocks of Bute, but found, deep down in
the lower grit, some beds which contained ealeareous matter, effer-
vescing readily with nitric acid.

§ 4. In descending from the antielinal axis of Ben Y-Happel
towards Loch Fyne, T found ridge after ridge unfolding precisely the
same series of micaceous grits, indurated sand, and gravel that [had
examined in Bute, in a similar state of metamorphism, all follow-
ing each other conformably, and dipping steadily to the N.W.; and
these grits continue all the way across to Otter, where there is a
thick bed of bluish hmestone, forming a small wooded hill, and quar-
ried beside the Otter Inn. This limestone is covered by quartz-rock,
and rests upon micaceous grit, and may be traced for some distance
along its N.E. strike. I believe it is also found near Kilfinnan ; and
I heard of some other seams or bands of limestone in Cowal—one
somewhere near Ardlamont Point, which would be on the strike of
the calcareous grit that I observed in Bute.

Again, in following the west shore of Loch Fyne from the neigh-
bourhood of the anticlinal axis in Cantyre north to Loch-Gilphead, the
strata all have a general dip to the N.W. I found, first the erumpled
coarse gneiss and mica-schist to the south of East Loch Tarbert,
gradually falling into more regular stratification towards Barmore,
near which a strong band of bluish limestone, quarried at Ashins,
and apparently the same as that of Otter, runs across to West Loch
Tarbert. After passimg Barmore the rock is very siliceous, and con-
tinues so all along the base of the lofty ridge of Shabh Goil on to

1860. ] : JAMIESON—S.W. HIGHLANDS, 139

Meal Dhu Point, the general character being a sort of granular
quartz-rock with little mica. Several large masses of greenstone
come out between the beds, and have crumpled them up, and in some
cases much altered their mineral texture, but do not seem to derange
the succession of the main body of the strata. At Meal Dhu Point,
or Strondoir, the rock assumes more mica, and continues to be mostly
micaceous with occasional beds of a more quartzy nature on to In-
verneil, where seams of green slate begin to show themselves and
become more and more numerous until they finally give the character
to the whole; and from Ardrishaig to Loch-Giulphead the rock all
consists of the thin-bedded green slates, much traversed by green-
stone, but dipping constantly to N.W. at low angles. Notwith-
standing the prevalence of these greenstones all along the shore here,
the passage of the lower grits into the base of the slate-series is
clearly indicated ; and some of the finely laminated green arenaceous
layers noticed near Kildavannan Point occur also in the correspond-
ing part of the section. {

Finding, however, no sections along the Crinan Canal to show the
upper part of the slates, I betook myself to the ridge of Cruach Lussa
(the highest hill in North Knapdale—according to the Admiralty
Chart 1530 feet), lying between Loch Fyne and Loch Swen, where I
found the passage of the slates into the upper grits well manifested
in the south-eastern flank of that mountain.

The base of the hill is here formed of a great thickness of these
finely laminated greenish slates, dipping N.W., at a high angle, into
the interior of the ridge; and as I ascended I found them pass up
into greenish grits, with several thick masses of bedded greenstone.
These appear to form all the upper part of the hill; but subordinate
slaty seams occur here and there, and one such finely laminated bed
passes over the very summit, enclosed between beds of grit and
greenstone. The N.W. brow of the hill shows thick strata of coarse
gravelly grit, perfectly identical with those in the upper grits of Bute,
and showing the same water-worn grains of bluish-hyaline and grey
quartz, of the size of peas or beans,—these beds all dipping to N.W.
at a very steep angle, accompanied by enormous masses of bedded
greenstone, which range from S8.W. to N.E. for miles, quite con-
formably to the strata.

Between Cruach Lussa and the Crinan Canal there is a barren
upland tract studded with tarns or little mountain-lochs, several of
which have been converted into reservoirs for the service of the
canal, This region is highly interesting in a geological point of
view, much of the rock being exposed, and showing great parallel
ridges of greenstone running along between thick beds of grit, with
some intercalated seams of slate and bluish limestone. At least
two beds of limestone occur in these upper grits here, but neither
of them so thick as that at Otter. They contain a good deal of sand,
and seem well adapted for the preservation of fossils ; and, although
I failed to find in them the slightest trace of organic life, I cannot
but think such will yet be found. There are also several finely
laminated schistose or slaty beds; but these are seen to be clearly

140 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Dec. 19,

subordinate to the grits, which, with the greenstones, form the
predominating features in the geology of this tract. From this to
the head of Loch Swen, the dip of the strata becomes nearer and
nearer to vertical ; and in the neighbourhood of that loch the general
position of the strata is almost upright, leaning occasionally to 8.E.,
and occasionally to N.W., but always striking from 8.W. to N.E.;
and to the west of Loch Swen the character seems to be a mere
repetition of those I have been describing. We find the same thick
beds of grit and greenstone, accompanied by subordinate seams of
slate and indications of limestone, still dipping at high angles; but
the inclination is now found to set in to 8.E. I therefore think that
here we have a synclinal trough whose axis lies in the direction of
Loch Swen; and, from the great apparent thickness of the strata,
even allowing for many repetitions, I conceive that we have in this
district a quantity of beds belonging to the upper grits beyond what
is found in Bute, where they terminate abruptly at the border of the
Old Red Sandstone.

§ 5, From the deseriptions and maps of Macculloch, in his capital
work on the geology of the Western Isles, it appears that the
easterly dip is maintained all through the islands of Shuna, Luing,
and Scarba, on to Jura, subsiding gradually to lower angles, and
exhibiting a descending series of grits and greenstones, followed by
clay-slate, mica-slate, and quartz-rock, in the very same order as I
have described them in Knapdale ; and, although I had not time to
visit those islands, I have little doubt that in the quartz-rock of
Jura we have the western extension of those great siliceous masses
that form the lofty ridges of Shabh Goil and Meal Dhu, between
Loch Tarbert and Loch Killisport. The clay-slate forming the
eastern border of Jura, and ranging north-east through Scarba,
Lunga, and Luing, on to Eisdale, I have as little hesitation in say-
ing, represents the slaty beds of Bute, which, rolling over the anti-
clinal fold, plunge under the upper grits of Cruach Lussa, and re-
appear again to the westward in the reversed curve, troughing, as it
were, these upper grits; and if the limestone of Islay, Garveloch,
and Lismore les at the base of the Jura quartz-rock, we have that
also paralleled by the calcareous masses of Otter, Barmore, and
West Loch Tarbert, which he beneath the quartz-rock of these
localities.

With regard to the thickness of these old rocks, taking either
side of the anticlinal axis, their enormous dimensions are equally
apparent. The mass of lower grits, judging from the Bute section,
must be many thousand feet thick; and the group of thin-bedded
slates in that island has an apparent thickness of 2000 or 3000
feet; while the upper grits, although far short of the dimensions
they seem to attain in Knapdale, form also a considerable body of
strata.

§$ 6. The greenstones, which I have so often mentioned, form a
most remarkable feature in the geology of Knapdale. They attain
their greatest development among the upper grits of the synclinal
trough, but are not confined to them, and alternate with the strata

1860. ] JAMIESON.—S.W. HIGHLANDS. 141

in huge parallel masses running from 8.W. to N.E. ; and to such an
extent are they developed in many places, as quite to overwhelm
the associated strata. From the fact of their being thus inter-
stratified with the slates and grits, Macculloch seems to have re-
garded them all as aqueous sedimentary masses ; for he has inserted
no trap or igneous rock in his map where they occur, and has
described them as a mere variety of chlorite-schist (see ‘ Western
Isles,’ vol. 11. p. 290). They are the typical beds of his ‘ chlorite-
series,” forming, as he says, nearly three-fourths of it ; and it is from
them that he has bestowed the name on the group,—quartz-rock
being ranked next in quantity.

I was unable, however, to perceive any character whereby they
could be distinguished from other greenstones: for they seem to be,
for the most part, composed of felspar and hornblende, and have
a massive form and crystalline structure hke syenite or granite ;
they may also be occasionally observed resting on the upturned
edges of the sedimentary strata; and finally, what seemed to me a
conclusive character, they have in many places exerted a powerful
metamorphic action on the adjoining strata. On the other hand, it
is difficult to conceive how they could be of an eruptive nature, or
be injected among the stratified beds posterior to their formation
without deranging the disposition of these to a far greater degree
than they have done: and, what is even still more singular, there
are many huge masses which seem to have exerted no metamorphic
effect whatever on the adjoming beds of grit, which display the
water-worn grains of quartz in a perfectly similar condition to
those of Bute, where no such greenstone is near them.

I have already mentioned that great quantities of greenstone come
out between the strata along the west shore of Loch Fyne, between
Barmore and Loch Gilp. One of these, near a place marked Muil-
more on the Admiralty Chart, is about sixty yards broad, and has
affected the quartz-strata on both sides, crumpling them up into
strongly wrinkled and corrugated masses, whose original greyish-
white colour has been changed into various hues of purple, red, and
yellow; and there are many segregations of vein-quartz, together
with streaks of a red colour strongly impregnated with iron-ore.
Their granular texture is also effaced, and they have become com-
pact and close-grained, like hornstone. The lamination and strati-
fication are in some places obliterated, and the rock traversed by
numerous fissures. At another spot, near Erins, I observed some
wedge-shaped masses of greenstone proceeding from the main body
and intruding amongst the quartz, where they thinned out into ten-
dril-like streaks. Near Meal Dhu Point another bed of greenstone,
30 or 40 yards thick, is seen coming out between the quartz-
strata, and powerfully affecting them on both sides to a distance of
about 20 yards. ‘The stratified rock is crumpled up, loses its ordi-
nary pale greenish-grey hue, and assumes a variegated colour of
red, ochrey-yellow, green, and brown, irregularly mingled; while
the lamination is in many places quite obliterated, and ravelled
veins of quartz ramify through it. Masses of the rock are con-

142 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

verted from a quartz-grit into compact jasper-lke or hornstone-
quartz. The greenstone itself is likewise affected, and traversed by
some very odd veins of quartz, which seem to proceed out of the
sedimentary rock. Various thinner beds of greenstone are seen
near these, interstratified with the quartz-rock and following its
undulations. Between Inverneil and Loch-Gilphead I noticed in-
stances where layers of mica-slate, followed along their strike, may
be seen gradually to assume a greenstone aspect; these micaceous
strata are also often much contorted in the neighbourhood of the
greenstone, which is itself occasionally altered and traversed by
cream-coloured veins. The action of the greenstone upon the thin-
bedded slates may be noticed in the low masses along the shore
near Ardrishaig Hotel. Sometimes it has caused a segregation of
the mineral ingredients, the quartz forming numerous white streaks
parallel to the bedding, together with some larger veins ramifying
in a more irregular manner; carbonate of lime has also in some
cases segregated along with the quartz; while the chlorite has also.
in a great measure been purged of its impurities, forming a tough
mass which has quite lost its laminated fissile character, and in
some cases it appears to pass imsensibly into the greenstone.
Although neither here nor elsewhere did I notice veins ramifying
from the greenstone, yet it has in some cases burst through the
strata transverse to the bedding, in good-sized masses. An instance
of this may be seen on the shore about halfway between Ardrishaig
and Loch-Gilphead, near a place marked Glenburn in the Admiralty
Chart, where some greenstone has protruded across the green slaty
strata, which become much crumpled as they approach it, and
assume an irregular sort of cleavage, or cross-planes of division ; they
also become more micaceous; and at some points the prolongation
of these micaceous slates passes insensibly into the greenstone
without any clear line of separation; there is, in short, a gradual
conversion of the slate into a massive greenstone ; but in other parts
the line of meeting is easily seen.

On the shore of Loch Fyne, to the north of Otter Ferry, near
a place marked Gortans in the Admiralty Chart, where green-
stone has invaded the quartz-strata and caused much alteration and
contortion in them, I observed a curious change in the greenstone
itself near its contact with the quartz, whereby it assumed a foli-
ated structure, and became highly micaceous—in short, took on the
aspect of a greenish mica-schist to the thickness of one or two
feet.

I observed likewise instances, both in Bute and Knapdale, where
dark fissile clay-slate is changed, near its contact with greenstone,
into a substance like basalt. On the line of the Crinan Canal,
between Dunartry and Ballenoch, a mass of greenstone is con-
spicuously seen, the weathered surface of which is full of circular
concretions like those often noticed in decomposing trap.

The chlorite-series has been laid down in the map of Macculloch
only in Argyleshire; this geologist therefore seems to have regarded
it as distinct from any of the other Scottish formations. Under

1860.] JAMIESON—S.W. HIGHLANDS, 143

this view we should have the singular fact of an immense succes-
sion of sedimentary strata developed here and nowhere else. This I
believe to have arisen from his having mistaken a trap-rock for an
aqueous sediment,

Another feature of the case even still more singular, if we should,
with Macculloch, hold these greenstones to be merely highly meta-
morphosed aqueous sediments, would be the fact of immense fel-
spathic and hornblendic beds alternating with others remarkable
for the absence of both these ingredients, and all deposited from the
same sea. It is easily understood how beds of grit should alternate
with slate and schist ; for the one is the sand, the other the mud
of the old sea-bottom, separated by the action of gravity ; but it
would be difficult to comprehend how the action of sea-water could
have sifted so finely grains of felspar from those of quartz, their
specific gravity being alike. In the Silurian rocks of Wales and
elsewhere, beds supposed to consist of contemporaneous trap or
voleanie ash are interstratified with ordinary aqueous sediment ;
and it is quite intelligible that felspathic matter from an igneous
source might be ejected at intervals, so as to be thus interstratified
with quartz-sand derived from the erosion of different materials ;
but in such cases the beds of igneous matter have been distinguished
from the ordinary aqueous deposits with which they are associated,
by a name marking their proper origin. Whether, therefore, these
greenstone-rocks of Knapdale are of contemporaneous formation
with the strata beside them, or whether they have been subsequently
injected amongst them, they ought in my opinion to be clearly di-
stinguished from the grits and clay-slates, and not classed under the
head of a mere variety of these, as they have been by Macculloch.
I prefer, then, using the term bedded greenstone, as marking this
distinction and, at the same time, indicating the fact of their alter-
nation with the stratified layers, as well as conveying a more just
idea of their mineralogical features.

I was unable to devote sufficient time for a thorough examination
of the district where these bedded greenstones occur, and would
recommend the locality to the attention of any geologist who may
have the opportunity, as likely to be well worth the labour of an
examination ; for it is very probable that here there may be green-
stones of different ages and various origin. I myself noticed some
vertical dykes of trap, of a blacker hue, which were evidently of a
later date, running in a N.W. direction, and cutting across both the
greenstone and grit, and causing alteration at the line of contact.
Two such may be seen in following up the course of the stream
that joins the Crinan Canal at Cairnbaan, and down which the tor-
rent descended when the reservoirs burst.

The fact of veins of lead-, copper-, and iron-ores being met with
in several parts of this greenstone-traversed district, is a circum-
stance characteristic of igneous action. In the micaceous strata to
the south-west of Inverneil I saw a lode or vein of white quartz, a
foot or more thick, which in many places is very rich in galena, fre-
quently accompanied by sulphuret of iron and copper. This vein

144 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

of quartz is also encrusted in some places with beautiful little ery-
stals of carbonate of iron or sparry iron-ore. Its course is nearly
vertical, with a strike about N. 25° W. It had been wrought in
former times as a mine, and is now opened anew. Other veins of a
similar nature, with some ironstone, are known to occur in the lower
grits between Inverneil and Barmore; and I heard that a vein of
lead had once been opened, at the rocky point between Loch Gilp
and Loch Fyne, and also near Dunartry, in the upper grits.

§ 7. I examined the limestones that came under my notice for
fossils, more particularly the thick calcareous grit of Otter, which
seemed a likely rock for containing them ; but in none did I perceive
anything of the kind. In the weathered surface of some of the
quartz-grits: in Knapdale, both above and below the slates, I noticed
numerous circular cavities, and also some curious elongated stripes
of coarser sand, which suggested the idea of iaeneddle burrows; L
could not, ihomeran 3 satisfy myself as to whether such was actually
their origin, and must leave it to the decision of those who know
more about these matters.

The period at which these old beds of sand and mud had been
thrown into undulations and changed into quartz-rock, mica-schist,
and slate is evidently very remote; for the Old Red Sandstone
conglomerate in the shore beside Rothesay is seen to be made up of
the débris of these strata; and it is important to remark that its
water-rolled pebbles of siliceous grit, mica-schist, and slate have
quite as metamorphic an appearance as the parent rocks from
whence they were derived have at the present day. Many of these
imbedded fragments show the same contorted, wrinkled, foliated
structure, and are traversed by the same ramifying veins of quartz
(which had solidified before the water-rolling of the fragments), and,
in short, are altogether identical in their mineral complexion with
the present features of the rocks I have been describing. Their
metamorphism must therefore have been completed before the Old
Red conglomerate began to accumulate; and this leads to the con-
clusion that a great chasm intervenes between the era when these
old rocks were formed and that of the Old Red Sandstone, and brings
us to assign to them a date anterior to that of the upper Silurian
beds. They do not appear to resemble, in mineral features at least,
either the ‘“‘ Cambrian sandstone,” or the “ fundamental gneiss ” of
Sir Roderick Murchison, described by him as occurring in the North-
west Highlands; while they seem to bear a striking resemblance to
the quartz-rocks, limestones, and mica-schists of Sutherlandshire, &e.,
shown by the same geologist to be of Lower Silurian age,—the chief
difference being the presence of the bedded greenstone, which, how-
ever, is, as I have shown, a local phenomenon, being absent in Bute,
So far, therefore, as lithological appearances are entitled to weight,
there is reason to believe them to be of similar date to those rocks of
the North-west Highlands. However, as mere mineral features
alone form a very unsafe criterion 1n snide cases, we must look either
for evidence proving the physical synchronism of these beds of
Argyleshire with the North-western types of Murchison, or, still

1860. } MITCHELL—OLD RED SANDSTONE. 145

better, for some clear fossil-evidence, before we can arrive at a
positive determination.

Perhaps the most interesting feature of the district described is
the immense development of these bedded greenstones, which may
serve as a parallel to the similar phenomenon in Wales; and to this
I would beg to draw the further attention of those interested in the
study of trap-rocks.

2. On the Posrrton of the Brps of the Orv Rep Sannsrone developed
in the Counties of Forrar and Kincarpine, Scortanp. By the
Rey. Hueu MircueEt.

[Communicated by the Secretary. |

§ 1. Tue time has now come for us safely to pronounce, from
paleontological evidence, upon the place of those fossiliferous flag-
stones, with their associated sandstones and conglomerates, which
are spread over a large territory in the counties of Forfar and Kin-
cardine, and which are referred to in a paper* read by Prof. Hark-
ness before the Geological Society on the 18th January of this
present year f.

The superficial area of country referred to in this paper is almost
the same as that in the paper of Prof. Harkness, namely a district,
comprehending all the lowland parts of the two counties, bounded
on the north by the Grampian Mountains, impinging on the west on
the County of Perth, and bounded on the south and east by the
German Ocean. The objects of the papers are, however, very different.
Prof. Harkness illustrated the stratigraphical arrangement of the
rocks by numerous sections along the northern boundary-line, where
they lean against the crystalline schists of the Grampians; our
attention is now directed more to the beds as spread out and ex-
hibited in the beautiful tract of country to the south-east of the
mountains, and which have of late years begun to yield not a few
characteristic and important fossils. It is now wished to state the
paleontological data, collected by the writer in the course of several
years, which lead to certain conclusions, in his opinion, sufficiently
determining the position and the importance of these rocks in the
geological scheme t.

* Entitled “ On the Association of the Lower Members of the Old Red Sand-
stone and the Metamorphic Rocks on the Southern Margin of the Grampians,”
Quart. Journ. Geol. Soc., vol. xvi. p. 312.

t See also a paper by the author “ On the Flagstones of Forfarshire,”’ ‘ Geo-
logist,’ 1859, vol. il. p. 147; his ‘“‘ Notice of New Fossils from the Lower Old
Red Sandstone of Scotland,” ‘Geologist,’ 1860, vol. iii. p. 273; and Mr. W.
Bes ee “On the Old Red Sandstone and its Fossil Fish in Forfarshire,”’
1d. P. Boo.

t The reader is referred to the 11th chapter of ‘Siluria,’ 2nd edit., 1859, for
the latest and most complete review of the history of the Old Red Sandstone,
and for the corrections made by Sir R. I. Murchison in the correlation of the
several members of this group. The Table at pp. 432 & 433 of ‘ Siluria’ gives a
general view of the classification adopted by Sir Roderick,—the Upper, Middle,
and Lower divisions of the Old Red Sandstone of Scotland being respectively

synchronized with different zones of the Old Red and Devonian rocks of Eng-
land and Europe.—Epir.

146 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dee. 19,

§ 2. Fossils occurring im the Lower Old Red of Forfar and Kin-
cardineshire.—With one exception (Stylonurus), which is in the pos-
session of Mr. Powrie, of Reswallie, the writer can produce from his
own cabinet the fossils enumerated in the annexed Table; but there
are still many undescribed Ichthyodorulites and separated scales of
fishes, which it is believed indicate other new genera and species.
There are also unnamed species (if not genera) of the family of the
Eurypteride among the Crustacea. It must not be forgotten that
in these rocks there is also a unique but fragmentary flora, of which
the only form at all resembling any recorded species is an organism
almost identical with that figured in plate 35. fig. 30 of ‘ Siluria,’
and which Dr. Hooker considers to be the spores of some cryptogamic
land-plant*. There are also forms in the author’s possession about
which only a conjecture can be hazarded. From one locality slabs
have been procured contaiming imprinted on their surfaces all the
phenomena of a sea-shore of the period—Annelide-tubes, Annelide-
tracks, a great variety of Crustacean tracks, rain-prints, and desic-~
cation-cracks.

o oO

al a os/38

& a Fossils occurring in the Lower Old Red Sandstone | 3E/ 35

ge] y of Forfar and Kincardineshire. es | m2

ae Bs AS | ies,

a Bs omtloe

Cc Pe os] od

Sales
See las

x |Cephalaspis . - : . *

Cephalaspis Lyellii, “Agass. 5 , . .|Abundant] *
Ptychacanthus dubius, Ag Igass. . : 4 : * *

# Acanthodes . : - - : * $00 || 23
Acanthodes Mitchelli, Fgert. : < Wee. .|Abundant.
Brachyacanthus scutiger, ayant - : *

Diplacanthus . * *
Diplacanthus, 2 spp. nov. *

* |Plectrodus : : < *

* |Onchus . . - : 5 * *
Onchus, 2 spp. nov. *

* Ctenacanthus . * *
Ctenacanthus, 2 spp. nov. %

Parexus incurvus, Agass. 2*
Climatius reticulatus, Agass. x
Stylonurus Powriensis, Page *
Kampecaris Forfariensis, Page *

x |Hurypterus - # *

* |Pterygotus : : : : * *
Pterygotus Anglicus, Agass A : ; _|Abundant.

x |Parka - ; . 4 so *
Parka decipiens, Flem. A ‘ 5 ; _|Abundant.
Vegetable remains . Abundant.

* Spores of a land-plant (Pach ytheca, Hooker) =

* Pachytheca, Hooker, MS. See also Quart. Journ. Geol. Soc. vol. ix. pp.
10 & 12; and ‘Siluria,’ 2nd edit. p. 267, note. —Enir.

1860. ] MITCHELL—OLD RED SANDSTONE. 147

On some of the fossils in the above list, a few brief remarks may
be allowed. Cephalaspis Lyelli, figured by Agassiz, is from Glammis,
Forfar; it is by nomeansrare. Ptychacanthus dubius appears, from
specimens in the writer’s possession and in the cabinet of Mr. Walter
M‘Nicol at Tealing, to be the posterior portion (serrated along the
inner margin) of the head-plate of a species of Cephalaspis.

The Acanthodian fishes are new to science, and are about to be
described by Sir Philip Egerton in a ‘ Decade’ of the Geological
Survey. Plectrodus has only recently been found here; and any day
the stroke of the hammer may expose to our examination the com-
plete form of this curious creature.

§ 3. The fossils connecting the Forfar and Kincardineshire beds
with the Upper beds of the Silurian System as developed in the
typical region of the latter, belong to the genera Cephalaspis, Plec-
trodus, and Onchus among the Fishes, and the genera Pterygotus and
Eurypterus among the Crustacea. There is also the curious organism
known as Parka. It may be questioned if our beds have one species
in common with the Ludlow rocks, although several genera seem to
range through both.

§ 4. The fossils connecting the Forfar and Kincardineshire beds
with the higher beds of the Old Red Sandstone belong to the genera
Acanthodes, Diplacanthus, and, in a sense, Ctenacanthus. Acan-
thodes rises into the Middle Old Red Sandstone, and is also found in
the Carboniferous rocks. Diplacanthus, if it be that genus which
occurs in the Lower, advances no further than the Middle Old Red.
Ctenacanthus, though not recorded from either the Middle or Upper
Old Red Sandstone, finds its way into the carboniferous rocks.

§ 5. The fossils occurring both in the Old Red Sandstone of
Herefordshire and in that of Forfar and Kincardineshire are
Cephalaspis Lyella and Ptychacanthus dubius, with the genera On-
chus, Otenacanthus, Pterygotus, Eurypterus, and Parka.

§ 6. With regard to the fossils peculiar to the Forfar and Kin-
eardineshire beds or to their equivalents in England, and deter-
mining them to belong to a distinct and well-marked zone of the
Old Red Sandstone, it may be said that the entire Fauna and Flora
are peculiar. There may be one or two doubtful cases, so far as
specific identity is concerned; but the facies is undoubtedly cha-
racteristic of the horizon of these beds. The genus Parka is highly
characteristic.

§ 7. Distribution of the Fossil Remains over the Counties of Forfar
and Kincardine.—Over this extensive area there is almost complete
identity in the fossil organisms. Of this some illustrations may be
given. Cephalaspis Lyellii has been found over the entire district
from Balruddery on the S.8.W., and on the confines of Perthshire, to
Canterland, close upon the German Ocean, in Kincardineshire—as at
these particular localities :—Balruddery, Tealing, Glammis, Carmylie,
Leysmill, Carsegownie, Brechin, and Canterland. The Acanthodian
Fishes are now known to occur in five localities:—Balruddery, Tealing,
Forfar, Farnell, and Canterland. These fishes were first detected by
the author in beds at Farnellin July 1857; but they are now turning

148 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dec. 19,

up over the whole district. Parexus incurvus is founded, by Agassiz,
on a very striking spine from Balruddery, but has also been detected
by me at Canterland, the other extremity of the district. Parka de-
cipiens, occasionally with an attached hgament or stem, or even with
what resembles a calyx or sheath, is universal, and abundant in
every section and in every quarry. Pterygotus is almost as widely
dispersed, though generally in a fragmentary condition ; and for it the
same localities may be stated as for Cephalaspis, with the exception
of Brechin, but substituting in place thereof Farnell, where plates of
the larger Crustaceans and complete forms of the smaller have been
found by the author and Mr. Powrie of Reswallie. Kampecaris was
described by Page from Balruddery, and has been found (perhaps
several species) by me at Canterland, the extreme of the area. Some
of the vegetable forms are generally diffused, like Parka decipiens,
occurring in every opening of the fossiliferous beds. Indeed the only
form, with the exception of the Crustacea (which are yet undescribed),
confined to one locality is Climatius reticulatus, recorded by Agassiz
from Balruddery ; but the genus is founded on a spine, and in the
multitude of our spines it might be easily passed over.

§ 8. Distribution of the Fossils through the vertical depth of the
Strata.—Though spread over a wide area, the arrangement of our
rocks is very simple. In the section at Canterland (which is typical
of the district) we have, first and lowest a gritty sandstone* (120 feet
seen), very ferruginous, and containing occasional thin layers of a
purplish flag ; secondly, grey flagstone with intercalated sandstones
(40 feet)+; and thirdly and above all, an overlying conglomerate+. A
similar life seems to have prevailed throughout the entire formation,
as embracing an era in geological time. We have met with a soli-
tary but well-preserved Parka decipiens§ far beneath the fossilife-
rous grey beds in the gritty sandstone which forms the bottom-rock
in the Canterland section. The Cephalaspis is found occasionally in
the sandstones used for building-purposes, as at Brechin (amme-
diately below the grey flagstones), in which, owing to the nature of the
matrix, not another organism is known. But whilst this is all the
direct paleontological evidence, there is other evidence of a physical
character. Among the purple flags, which lie very low in the for-
mation, there have been gathered slabs containing on their surfaces
impressions, numerous and well marked, of what we may call the
phenomena of a sea-shore of this palzozoic epoch. On that sea-
shore the tides must have ebbed and flowed, the rain have fallen, now
in heavy shower, anon in drizzling mist, the sun must at times have
shone with sultry beam, and many creatures have travelled across
the palimpsest surface. Besides the Annelide-markings, we have

* Judging from the dip and the neighbouring rocks, this sandstone probably
rests on a dark-red sandstone.

t In the quarries at Carmylie these are 120 feet thick.

¢ A few feet thick here, but several hundred feet thick as it rises up the neigh-
bouring hills. At the Hill of Turin, conglomerate (2 feet thick) is intercalated
amongst the grey flagstones.

§ Sir R. I. Murchison and Mr. Powrie found the Parka decipiens common in
the lower conglomerates on the mountain or western flank of the basin.—Ebrr.

1860. ] MITCHELL—OLD RED SANDSTONE. 149
counted at least eight forms of Crustacean tracks, indicating an assem-
blage at the time, on that ancient sea-beach, of creatures similar in
size and organization to their congeners preserved in higher beds of
the formation, namely the grey flagstones. Although the number of
limbs attached to these ancient Crustaceans may still be matter of
doubt, yet we have in their stone impressions such a character as
would, on the one hand, be made by a gigantic Pterygotus, and on
the other, such as would be made by a creature as small as the
Sandhopper of our present shores, besides various intermediate forms
corresponding with the remains found in the flagstones. From such
evidence (and we think it must be allowed) do we infer the existence
of a similar life throughout the formation, even when all trace of the
organism has itself perished.

OLD RED SANDSTONE.

Upper . Holoptychius-beds of Moray, Perth, and Fife.
Middle . Fish-beds of Cromarty and Caithness.
( Conglomerate.
| [Canterland Den.]
Grey flagstone with
intercalatedsand- ; 4
a Cephalaspis Lyellit.
anes a Ichthyodorulites.
[Coptorlond “Den | Acanthodian fishes
( A ie ny eae Pterygotus Anglicus.
hee 190 nee Kampecaris Forfariensis.
Lower (10,000 fot Carmylie), near Vcectableiremains, dc:

thick in Forfar) . Farnell, &c.]

Gritty ferruginous

sandstone, with

occasional thin | Cephalaspis (in sandstone at Brechin).
| — layers of purplish Ripple-marks, Rain-prints, Worm-

flagstone. markings, Crustacean tracks (large

[Canterland Den and small, on the flags).

(120 feet here | Parka decipiens (in the lowest grit*).

seen), Ferryden,

&e. |

§ 9. Some of the general conclusions to which the paleonto-
logical data seem to lead us may be stated as follow :—

First, it must be granted that in these beds developed in the counties
of Forfar and Kincardine in Scotland, and their equivalents in England,
we have the lowest members of the Old Red Sandstone. We do not
venture to determine what those metamorphic rocks are upon which, on
the western side of our district, the Old Red Sandstone rests ; we leave
that point for future decision, either by the discovery of fossils in
some part of the Grampian chain or by the clear unfolding of their
stratigraphical relations. We hold, however, that the position of
the beds the paleontology of which we have here endeavoured to
describe may now be held as fully ascertained. They are the foun-

* And also in layers which alternate with coarse lower conglomerates on the
S.E. flank of the Grampians.—Hpir,
VOL. XVII.—PART I. M

150 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Dece. 19,

dation of that great series of rocks which for our northern land was
first described by Sedgwick and Murchison, and since rendered clas-
sical in the literature of the age by the writings of Hugh Miller.
Though it is matter of doubt if any one of the species found in these
beds occurs in the system beneath, yet there are genera in common.
There are thus links binding them without a gap to the past stage
of life and its conditions. Still, in the abundance and variety of the
fish-remains, and in the introduction of new forms, as well as in the
tokens of a terrestrial surface, we feel that we have entered into a new
epoch and anew domain of created existence. There has been in
some minds a hesitation to accept these rocks as the basis of the
system; but we think the evidence adduced is conclusive on this
oint.

: Secondly, the review of the peculiar fauna and flora of these
lower beds of the Old Red Sandstone affirms the necessity of subdi-
viding the system into formations, and of assigning to the Forfarshire
flagstones (with their associated sandstones, cherty limestones, and
conglomerates) the place of the Lower formation in this extensive
group of strata. The thickness of our Forfarshire beds is enormous,
10,000 feet at least. In these rocks we have a facies of animal and
of vegetable life characteristic and distinct from that of the Upper
and Middle formations; a subdivision is therefore demanded for
the purposes of classification. Between the Lower and Middle and
Upper beds of the system, there is a marked hiatus : for Cephalaspis
has never yet been found but in the Lower formation ; and when we
leave that, not only is Crustacean life at once and immensely dimi-
nished in its numbers, but its types are completely changed.

From the recorded observations of Mr. Geikie, there seem to be
other areas, of great extent, in Scotland over which this Lower Old
Red Sandstone is known to spread; and its area in England is very
considerable. We have thus all the elements of value in constituting
a formation in geological classification, namely superficial develop-
ment over extensive areas, great (we may say enormous) depth of
strata, considerable variety of mineral conditions (in conglomerates,
flagstones, sandstones, and cherty limestones), and a peculiar paleon-
tology.

Thirdly, we claim the right of the Old Red Sandstone as a whole
to be admitted and fully recognized as one of the great systems in
geology, both on the ground of what has been now advanced and
from all previously recorded knowledge of the Middle and Upper
formations. The series of rocks called the “ Old Red Sandstone ” is
as large as almost any of the well-marked and acknowledged divisions
into which, at the call of Science, the strata of the earth have been
made to fall. The system in Scotland alone covers an immense extent
of ground. There are large patches of it flanking the Silurian strata
in the south of Scotland—in Berwickshire, Roxburghshire, Lanarkshire,
and Ayrshire. There is the great development of it in the central
district of Scotland, comprehending all the lowland portions of Kin-
cardineshire, Forfarshire, Perthshire, Stirling, and Dumbartonshire,
with many an offshoot into neighbouring counties. It stretches on

1860. ] BRODIE—LIASSIC CORALS. 1G

the east far out into the German Ocean, as we know by the Bell
Rock. We have tracts of the Old Red, more or less continuous,
along the shores of Aberdeenshire, Banffshire, Moray, Nairn, Inver-
ness, Cromarty, and Caithness—covering this entire county and then
grasping all the Orkneys inits wide embrace, and stretching out even
to the remote Shetlands.

It is quite possible that some of the Old Red beds north of the
Grampians were laid down contemporaneously with the beds to the
south, and therefore that we have in the respective faunas or floras
of both a life existing in the same era, but placed in different regions
and in somewhat different conditions. But, even after this reduction
of the vertical depth of the entire system, there would yet remain
two great divisions, an Upper and a Lower, which cannot be put
into parallel ages. If our interpretation of the obscure vegetable
remains and the sea-shore-markings be correct, we have, from the
very commencement of the era of the Old Red Sandstone, indications
of the existence of land-surfaces ; while in the waters there was such
an abundance of piscine life as to mark the period, throughout, as one
of the most memorable in the past history of our globe.

January 9, 1861.

William Charles Lucy, Esq., Gloucester ; Robert Dukinfield Dar-
bishire, Esq., B.A., 1 Heald Grove, Rusholme, Manchester ; George
Charles Wallich, M.D., 17 Campden Hill Road, Kensington, were
elected Fellows.

The following communications were read :—

1. On the Distribution of the Corats in the Las. By the Rev. P. B.
Broprg, M.A., F.G.S.

[ Abstract. ]

From observations made by himself and others, the author was en-
abled to give the following notes:—In the Upper Lias some Corals
of the genera Thecocyathus and T'rrochocyathus occur. The Middle
Lias of Byfield, Northamptonshire, and Ilminster, Somersetshire, has
yielded a few Corals. The uppermost band of the Lower Lias, viz.
the zone with Ammonites raricostatus and Hippopodium ponderosum,
contains a Thecocyathus, numerous at Cheltenham and Honeybourne
in Gloucestershire ; and a Montlivaltia in considerable abundance at
Down Atherley in Gloucestershire, at Fenny Compton in Warwick-
shire, and more rare at Aston Magna in Worcestershire, and at Kilsby
Tunnel in Northamptonshire. The middle members of the Lower
Lias appear to be destitute of Corals. In the zone with Ammonites
Bucklandi, called also the Lima-beds, a Cladophylha is found at
Down Hatherley and Bushley in Gloucestershire ; and in the same
beds at Inkberrow, Evesham, Binton, Wilmcote, and Harbury, in
M 2

152 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 9,

Warwickshire, and at Shepton-Mallet in Somersetshire, an Isastraa
occurs. Dr. Wright states that Jsastrea Murchison has been met
with in the next lowest bed of the Lower Lias, namely the White
lias, with Ammonites Planorbis at Street in Somerset ; and another
Coral has been found in the same zone at Whitnash and Itchington
in Warwickshire. Lastly, in the ‘“‘Guinea-bed ” or “‘ Guineas” at
Binton in Warwickshire another Coral has been met with.

The Montlivaltie of the Hippopodium-bed and the Jsastrece of the
lima-beds appear to have grown over much larger areas in the
Liassic sea than the other Corals here referred to.

2. On the Sucrions of the Matvern and Leppury Tunnets (Wor-
cusTER and Hernrorp Rarnway), and the intervening Line of
Railroad. By the Rev. W. 8. Symonps, F.G.8., and Aran Lam-
BERT, Esq. With a Note on the Fosstts; by J. W. Sarrer, Hsq.,
F.G.8., of the Geological Survey of Great Britain.

Iy a paper published in the Edinburgh New Philosophical Journal
for April 1857 (p. 257), I described briefly the “Correlation of the
Triassic Rocks in the Vale of Worcester and at the Malvern
Tunnel.” These rocks have the following order on the flanks of the
Malverns :—

Upper Keuper Marls.

Upper Keuper Sandstone.

Lower Red or Keuper Marls.

Lower Keuper Sandstones (Waterstones).

Upper Red Sandstone (Bromesberrow beds).

Lower Red Sandstone (Stourport beds).

No. 6. The lowest of these deposits is a dark-red sandstone with
black patches, and closely resembles the “ Lower Red Sandstone”
of the geological surveyors in mineralogical character. It is to be
seen at the back of the stables of the Belle Vue Hotel at Great Mal-
vern, dipping from the hill, to the south-east, at an angle of 60°.

A large erratic block, angular and with no sign of subaqueous
action, was found imbedded in this dark-red sandstone. This
erratic block is different to any rock now exposed in the Malvern
district, and appears to me to belong to the Cambrian grits of North
Wales, or possibly to that of the Longmynd. It may be seen in
the Museum of the Malvern Field-Club at the Messrs. Burrow’s,
Great Malvern.

No. 5. This Upper Red Sandstone (Bromesberrow beds) may be
studied with advantage at the village of Bromesberrow, where it
overlies the Haffield or Permian breccia of Prof. Ramsay and the
Geological Survey Map, and is covered by the Waterstones of the
Newent district.

No. 4. Lower Keuper Sandstones (Waterstones).

A patch of these sandstones flanks the Chase End Hill of the
Southern Malverns, and ranges from a wood at the back of the
Hawthorns, in the parish of Berrow, towards Bromesberrow Place,

zy cos ocr aoe te

a

1861.] | sYMONDS AND LAMBERT—MALVERN AND LEDBURY. 153

the seat of Mr. Osman Ricardo, M.P. for Worcester. Again they
may be seen covering the Bromesberrow sandstones near the Glynch
Brook, and ranging south towards Red Marley D’Abitot, where
they are faulted against the Lower Keuper Marls, which should
surmount them.

No. 3. Lower Red Marls.

These soft marly beds are well exposed in the lateral valleys in
the Malvern district. These are valleys of denudation, and in most
instances occur where anticlinals of Keuper Sandstone have been
broken and the apices or ridges of the anticlinals removed.

No. 2. Upper Keuper Sandstones.

These fossiliferous sandstones have been generally denuded along
the Malvern Vale. Wherever I have studied them, they are mere
relics of a series of low anticlinals.

No. 1. Upper Grey and Red Mazrls.

These rocks are the uppermost Triassic deposits, and at the Ber-
row Hill, within two miles of the Chase end of the Malvern ridge,
pass upwards conformably into the Lower Lias, with the charac-
teristic fossils.

I now refer to the section of the tunnel at Malvern Wells, on the
Worcester and Hereford Railway, prepared by Mr. Alan Lambert
and myself, and for the admeasurements of which I am indebted to
Mr. Lambert, one of the engineers upon the line, who has assisted
me throughout this somewhat arduous undertaking with the utmost
courtesy and good will. Mr. Lambert has prepared a section (re-
duced in fig. 1) of the line of railway, from the entrance of the
Malvern tunnel to the exit of the Ledbury tunnel on the Hereford
line, for the Geological Society of London, at the request of Mr. Lid-
dell, the chief engineer of the railroad.

The entrance of the tunnel (see Section, fig. 1, and the Expla-
nation) commences with the Upper Keuper Marls (10 m. 330 yds.),
overlain by a considerable thickness of subangular drift, which has
furnished the bones and teeth of Bos primigenius, of Hlephas primi-
genius, and of Lhinoceros tichorhinus. The site where these mam-
malian relics were discovered is near the Station at Malvern Wells.
Some of these fossils are in my possession, and some are at Worcester
Museum. The Upper Keuper Marls at the tunnel’s mouth have
been much denuded. In the tunnel they pass into the Keuper Sand-
stones and Marls with the Hstheria and fragments of teeth and spines
of Lophodus (formerly Acrodus).

These deposits are much broken and contorted, and pass into a
series of red marls, which, I do not doubt, are the representatives of
the Lower Keuper Marls (10 m. 550 yds. to 704 yds.).

The Lower Keuper Marls dip away from a syenitic and brec-
ciated rock, against which they rest conformably at an angle of 50°.

It is worthy of observation that the Lower Keuper Sandstones
(Waterstones) and the Red Sandstones of Bromesberrow are en-
tirely wanting in the tunnel. I was puzzled, at first, whether or
not to rank the brecciated syenite as an equivalent of the Haftield
Permian breccia, as there is evidence of stratification. The stratifi-

ite i it

Fig. 1.—Section on the Worcester and Hereford Railroad, beginning at 10 miles 330 yards from Worcester, and ending at
“ )

o> Hast.
I
>
jL=4j
Malvern Tunnel.
e F i Tiga ira a via are ail =a
a | ‘ eee iret et ieee oliepaeltino eal | | et
iS | g Hse tsa cate mee wie eat |
g © cee eas 8 ase ge get sf 3 |
iS 1 ms 4 Ih I a N
S \ eal oreeg tiaat beeline Uae a © pire ec. 8 .
i N ie ee a eee na . y : i
S| N 8 RK GaenaeaN m N =
i) S S Q SI S$ S N
rs NI) K\ g S s
: ‘ ‘2
Z : s 8
o S es ay e Qq
\ pRiet 82 : S
2 | eee S§ RR
SS
djs 2 : = ae
fy « OLD RED MARLS == be =
: : DRIFT 0
a . :
3 S
B 3
=|
oO
Fe
2 West.
Ledbur
DRIFT y
UPPER LUDLOW ROCK aaa
: . NS
x OT T Falta T 7 7 - = -
2B | relate se eo ea lev ie a
Eo dy é H 1 (he Cea eT H Pict | |
a ! ' ‘ ! mea tics Y It 1 ! | i m
a \ H \ x \ 1 18 uy ? ' | 9 Gy! 8 °
: § ee eR al SI eat eer hae SS g
S & 3 q 2 8 A S FAULT R in hyarerey
< iS is ; J
N ~ a
5 SS)

Scale 500 yards to the inch, horizontal: 160 yards to the inch, vertical.

1861. ]

SYMONDS AND LAMBERT—-MALVERN AND LEDBURY. 155

Explanation of the Geological Section on the Worcester and Hereford
Railroad, from 10 miles 330 yards from Worcester to 15 miles
1463 yards.—See Fig. 1.

Miles. yds.

At

From

At

At about
Up to
At
From
At about

From
At

From
At

10 330. Keuper Marls, red with grey bands.
», 9000. Tunnel commences.
550. to 10 m. 704 yds. Keuper marls and sandstone, twisted and
broken; sometimes nearly horizontal, and sometimes with
a dip of 50°.
704. Syenitic breccia and thin band of black schist: dipping at
an angle of 58° towards the hill.
» 711. Syenite.
792. Thin band of chlorite, with black schist in contact.
,», 8836. Chlorite, with syenite caught up.
5, 9858. Syenite.
5, 909.:Greenstone.
» 925. Syenite.*
,, 946. Greenstone.
1012. Black hornblendic rock, with highly crystallized felspar, with
overlying greenstone.
,, 1057. Syenite.
1159. Two thin bands of Llandovery limestone, about 6 in. thick,
with 2 ft. of marl.
,, 1160. Syenite.
1254, Llandovery shales and limestone in thin bands, pressed against
syenite; syenite overhanging.
,, 1820. Woolhope shales.
,», 1436. Woolhope limestone.
», 1449. Wenlock shales and thin bands of sandstone.
11 260. Wenlock limestone (thickness uncertain).
,, 440. Lower Ludlow shales.
440. Old Red marls, with thin bands of grey and red sandstones.
», 1012 to about 18m. Local drift and red marls.
13-0. _Ludlow rock.
44, Old Red, lying unconformably against Ludlow rock.
fe 44 to 14 m. 352 yds. Local drift and red mars.
14 352. Upper Ludlow rock.
880. Old Red marls.
1144. Upper Ludlow rock.
,, 1298. Aymestry rock.
1342. Lower Ludlow rock.
1480. Local drift, 40 ft. thick, overlying drift derived from Old Red
Marl: Lower Ludlow rock beneath.
1518. Upper Ludlow rock.
, 1600. Aymestry rock.
1600 to 15 m. 406 yds. Ludlow and Wenlock shales.
15 406. Wenlock limestone, horizontal.
572. Lower Ludlow rock, angle 12°, north, passing at about 886
yards to 75°, south.
957. Aymestry rock, angle 75°, south.
, 1029. Upper Ludlow shales, angle 75°.
,, 1087. Downton sandstone, angle 75°.
,, 1091. Passage-beds into the Old Red Sandstone, angle 75° ; thin
bands of grey and red sandstones.
,, 1186. Tunnel’s mouth.
,, 1463. Section ends.

”

9

9

a3

’
’

156 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Jan. 9,

cation, however, is but partial, and I am inclined to look upon the
brecciated rock as-a portion of an ancient beach or talus derived
from the syenitic ridge. We observed a thin band of black horn-
blendic schist in contact with the syenitic breccia; and both these
rocks have undergone so much derangement as to dip at an angle
of 58° into the hill.

On reference to the section, we find a mass of syenite (at 10 m.
711 yds.) constituting the external walls of a nucleus which forms
the centre of the Malvern range, and which nucleus is of great
interest to the geologist and mineralogist. The thickness of the
syenitic crust on the eastern side of the Malverns is 125 yards. It
is much broken, and will require bricking and roofing in the tunnel.

Traversing the syenite, we found a bed of chloritic rock (at 10 m.
792 yds.) with a vein of shining, coal-black, graphite-looking schist
in contact, see fig. 2. Another wall of syenite is succeeded by a

Fig. 2.—Section in the Mal- Fig. 3.—Section im the Mal-
vern Tunnel, showing veins of vern Tunnel, showing veins of
Quartz and Graphite in the band = Felspar in the Greenstone over-
of Chlorite in the Syenite,at10m. lying black hornblendic or droritic
792 yds. By Capt. Selwyn. rock, at 10 m. 1012 yards. By
Capt. Selwyn.

O\\ 7 ee, Sail
iMUCor< oo fe
b a LAL IZ, a
eS SS
eS

z _ — ARB { \ }

a, Syenite. ‘
é. Greenstone and Felspar-yeins.
ce. Hornblendic rock,

vein of chlorite with highly crystallized bands of syenite. Here |
the syenite again sets in in a solid mass, and we pass onwards to a
mass of greenstone (10 m. 909 yds.) of the hardest material, and
160 yards thick. The greenstone appeared to me to have been
injected when fluid into a fissure in the syenite, the syenite being
fissured in a line with the range of the Malverns. It is worthy of
remark that the syenitic rock is much crystallized where it is in
contact with greenstone.

Leaving this mass of greenstone, we find a remarkable black and
greenish rock (hornblendic), containing many veins of red felspar.
It has greenstone on both sides. This great amount of change in
mineral structure in so narrow a compass could hardly have been
imagined, had not the interior of the Malverns been laid open to
our investigation. See fig. 3.

We pass next into a strong rock of syenite (10 m. 1037 yds.),
147 yards in thickness, and which we may consider as the external

1861.] | syMoNDS AND LAMBERT—MALVERN AND LEDBURY, 157

western crust of the Malvern plutonic range. We were astonished
to find, almost in the centre of this solid syenite (for the syenite on
the western side is not nearly so much shattered as that on the east-
ern flank), two thin bands of Llandovery limestone, with strata of
marly shales 2 feet thick lying in a fissure of the syenite. Fig. 4,

Fig. 4.—Section in the Malvern Tun- Fig. 5.—Section in the
nel, showing a seam of Llandovery rock Malvern Tunnel, showing
in the Syenite, at 10 m. 1254 yds. By the Junctionof the Silurian
Capt. Selwyn. rock and the Syenite, at

10 m. 1254 yds. By Capt.

L. Llandovery shales and lime-
stones.
S. Syenite.

1 Shale. 2 Limestone.

This Llandovery limestone (formerly ‘‘Caradoc’”’ of Murchison) con-
tains some characteristic fossils; and the shales have furnished a
Pentamerus. Neither the limestone nor shales are in the slightest
degree metamorphosed. The fissure runs from north to south, and
becomes smaller towards the south. These sedimentary deposits were
evidently deposited in a fissure in the syenite during that far distant
epoch when the waves of the Upper Llandovery seas washed above
the syenitic ridge of the Malverns, and when this interesting and
instructive range of hills was a low submarine ridge, of plutonic origin,
and of which the syenitic crust was, even in the Upper Llandovery
epoch, as much cooled, consolidated, and mineralized as at present.
I mentioned that the Lower Keuper sandstones, the Bromesberrow
sandstones, and the Haffield Permian breccia (?), which are all to be
seen at the southern extremity of the Malverns, are wanting in the
tunnel on the eastern or Worcester side of the Malverns. It is
somewhat remarkable, also, to find that the Cambrian (Holly-Bush)
sandstones and Lingula-flags (black shales) of the Chase End,
Ragged Stone, and Midsummer Hills (South Malverns) should be alto-
gether absent on the western flank of the hills of the Wells. The
syenite passed, we find limestones and shales, of the Upper Llando-
very epoch, full of fossils, resting perpendicularly against the ex-
ternal wall of syenite. Fig.5. We have evidences of great pressure
and crushing, but not a symptom of metamorphism; and I exhibit
a portion of shale, containing the Pentamerus levis, which was ob-
tained by Captain Peyton close to the line of junction. The Rev.
Reginald Hill, of Bromesberrow, Hon. Secretary to the Malvern
Field-Club, was the first to disinter these fossils of the Llandovery

158 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 9,

rock from their long resting-place ; and to him, to Captain Peyton,
of the Bartons, Ledbury, and to Captain Selwyn, I would express my
kind acknowledgments for their assistance in unravelling the secrets
of the Malvern tunnel.

It is difficult to ascertain the thickness of the Upper Llandovery
rocks here (10 m. 1254 yds.), or to determine any line between
them and the overlying shales; they are conformable, and pass one
into the other without any perceptible change, excepting in their
colour, as, from a purplish grey, they change into a blue mass of
shales with thin bands of limestone and grey and brown sand-
stones. Ihave thought it necessary, however, to draw a distinction
between the Llandovery rocks which rest against the syenite and
contain purplish shales with Pentameri, and the shales that underlie
the Woolhope limestone, because at a certain point I found the Penta-
merus-shales were overlain by a sandstone also containing Llandovery
fossils, but which is the rock formerly known as the ‘‘Caradoc sand-
stone of the Malverns,” underlying the Eastnor Obelisk and cropping
out along Howler’s Heath. At this point of the section, therefore,
I have drawn a somewhat arbitrary line, and have designated the
shales above this sandstone as Woolhope shales (10m. 1320 yds.).
Dr. Grindrod, of Malvern, has a fine collection of fossils from these
Woolhope shales, and also some splendid slabs with Pentameri from
the Llandovery shales.

The Woolhope. limestone (10 m. 1436 yds.) is quarried in the
tunnel within a short distance of the shaft No.2; and we then
pass on into the well-known Wenlock shales (10 m. 1449 yds.).
The distance from the Woolhope limestone to the pomt where the
Llandovery rocks rest against the syenitic ridge is nearly 200 yards ;
and it is therefore evident that the sedimentary rocks were deposited
at this particular point of the Malverns in a Little bay, or coomb, in
the syenite. This peculiarity was pointed out to me several years
since by my late friend Mr. Hugh Strickland.

From shaft No. 2 to the mouth of the tunnel on the Ledbury or
western side of the Malverns, the railroad passes through Wenlock
shales, and strikes the Wenlock limestone (11 m. 260 yds.) at the
distance of about 260 yards from shaft No. 2. Here we have evi-
dences of a considerable fault: near the tunnel-mouth (11m. 352 yds.)
the Wenlock limestone is thrown down horizontally, the greater part
of the Lower Ludlow rock is wanting, the whole of the Aymestry
limestone and the Upper Ludlow shales are deficient, and some sand-
stones and marls of the Old Red series (and these certainly not the
lowest Old Red deposits) are faulted agaist a regular “scrunch ”
(to use a miners’ phrase) of the Lower Ludlow clays. The Malvern
greenstone was not so difficult to work (as I have been assured by
Mr. Ballard, the contractor) as this ‘jammed and scrunched clay”
(11 m. 440 yds.).

From hence the railroad passes, for a considerable distance, over
red clays and marls covered with local drift; and there is nothing
worthy of attention until we reach the road that leads from Colwall
to Ledbury. In the lane ascending towards The Bartons, the seat

1861.] | symonDs AND LAMBERT—MALVERN AND LEDBURY. 159

of Mrs. Peyton, we see the Upper Ludlow shales dipping towards the
yale in which the railroad runs. At the base of the hill is a bridge
constructed for railroad-purposes, and at this spot the workmen
quarried the Auchenaspis-grits of the Lower Old Red Sandstone,
placed, at an angle of seventy degrees, on the clays of the Upper
Ludlow, and reversed*, On reference to the Ledbury section, it
will be seen that there is a great thickness of rock between the
Auchenaspis-grits and the Upper Ludlow shales.

For some distance the railroad cuts through local drift, until, a
short distance after crossing the highroad from Worcester to Led-
bury, we pass through a section of Upper Ludlow rock, with
abundance of characteristic fossils (13 m. 352 yds.).

We have next a small basin in which, besides the local Silurian
drift, there is a mass of red and grey clays, evidently derived from
the denudation of the Old Red Sandstone (13 m. 880 yds.).

The railroad again strikes the Upper Ludlow shales, rising from
a short synclinal, and passes through a section of the Aymestry
limestone and a portion of the Lower Ludlow shales, which are
overlain, near the eastern entrance to the Ledbury tunnel, by a con-
siderable thickness of red and grey stratified drift derived from
Silurian and Old Red deposits (from 13 m. 1144 yds. to 1518 yds.).

This drift appears to me to be one of the most important points
with which we have to deal. Bones of Mammalia have been de-
tected therein, and amongst them the tooth of Rhinoceros tichorhinus.
This evidence surely tends to prove that the Old Red Sandstone
covered the Upper Silurians of the Ledbury vales as late as the
Pleistocene epoch, and that it was removed by the action of Pleisto-
cene waters, which denuded the Old Red Sandstone, and redeposited
its débris with the relics of animals that lived on the land.

The tunnel proceeds through the Lower Ludlow shales at 138 m.
1430 yds., and then a fault occurs. The Upper Ludlow shales, with
the Aymestry rock, are quarried near Shaft No. 1 of the Ledbury
tunnel. The accompanying Section, fig. 6, furnished by Mr. A.
Lambert, supplies us with the details of the fault as seen in the tunnel.

Fig. 6.—Section in Ledbury Tunnel, showing the Fault,
at 13 m. 1518 yds. By A. Lambert, Esq.

Aymestry
Rock. 70°

Wenlock Shale. Ww,

1 Lower | Lower
} Ludlow ! Ludlow
Roc i Rock.

Wenlock Shale. t

—<$<$<——$ ——————————

BSA
66 feet.

——’ S——
18 feet. 18 feet.

* T have to thank my friend Captain Peyton for directing my attention to this
interesting fault.

160 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 9,

We descended Shaft No. 2, and examined the tunnel right and
left. Shaft No. 2 is in the Wenlock shales; these are seen to
pass into the Wenlock limestone (14 m. 406 yds.), which is thrown.
down, and is horizontal. A glance at the section will explain the
extraordinary faulting of the rocks between Shaft No. 2 and the
Lower Ludlow rock and the point on the section where the strata
incline at an angle of 75°, which dip continues to the western exit of
the tunnel, throughout the Lower Ludlow shales, Aymestry rock,
Upper Ludlow shales, Downton sandstone, red and mottled marls,
grey shales and grits, and purple shales and sandstones, the tunnel
ending at the point where the red and grey Auchenaspis-beds pass
conformably into the underlying strata*.

The following is the ascending order of the beds observed in the
section from 14 m. 957 yds. to 1463 yds.:—1. Aymestry rock with
Pentamerus Knightii, &c. (10 feet). 2. Upper Ludlow rock with
Chonetes lata, &c. (140 feet). The Ludlow bone-bed seems to be
wanting here. 3. Downton bed, thin (9 feet), with Lingula. 4 to8.
Red and mottled marls and thin sandstone (210 feet), with Lingula
and Pteraspis. 9. Grey shale and thin grit (8 feet), with Cepha-
laspis and Pterygotus. 10 and 11. Purple shales and thin sand-
stones (34 feet). 12. Grey marl passing into red and grey marl
and bluish-grey rock (20 feet), with Auchenaspis, Plectrodus, Cepha-.
laspis, Onchus, Pterygotus Ludensis, Lingula, anda Lituite (?). These
pass upwards conformably into a series of red marls, with yellowish
grey and pink sandstone containing Pteraspis and Cephalaspis, and
undoubtedly forming the base of the Cornstone-series of the Old
Red Sandstone.

With the exception of colour, there is no possible means of draw-
ing any line of demarcation bere between the Upper Silurian de-
posits and the lowest rocks of the Old Red Sandstone. Fossils dimi-
nish in number in the Old Red, it is true; but it is evident that this
is either owing to the change that occurred in the physical con-
ditions of the sea, or because the chemical condition of the deposits
was unfavourable to their preservation. As it is, we have a Lingula
common to the Downton beds and the Lower Old Red; while Ce-
phalaspidian fishes, beginning in the Silurian (Lower Ludlow), con-
tinue upwards into the Old Red.

The section from Malvern to Ledbury is most instructive and
most gratifying ; for we, who have followed in the wake of Murchi-
son, Strickland, Phillips, and the father of Malvern geology, the
present President of the Geological Society (Mr. Leonard Horner),
have learned upon how firm and scientific a basis the investigations
of these philosophers were founded, and how little we have been
enabled to add to the superstructure by later researches.

* See the author’s paper on the Ledbury Tunnel, Quart. Journ. Geol. Soe.
vol. xvi. p. 193.

1861. ] SALTER—SILURIAN FOSSILS. 161

Note on the Fosstzs found in the Worcester and HErErorD
Rattway Currines. By J. W. Satrer, Esq., F.G.S.

[In a Letter to the Rev. W. 8. Symonds, F.G.S.]

Tae tunnel through the hill (near Malvern) has given me a better
idea of the Woolhope beds than I ever had before. The quantity of
fossils is extraordinary. Our own collector, Mr. Gibbs, of the Geolo-
gical Survey, Dr. R. B. Grindrod of Malvern, and other friends have
obtained a great many, and in the most perfect state of preservation.
Of Corals there are only a few—the ordinary Wenlock species (for
the Woolhope limestone is nothing else than a lower Wenlock rock).
Of Cystideee the little Echinoencrinus armatus is frequent enough.
Trilobites are abundant. Jllenus Barriensis attained its full size
here. The strawberry-headed Trilobites (Zncrinurus) are in great
perfection, also Cheirurus, Spherexochus mirus with its globular
head, Acidaspis, Iichas, and four species of Phacops, including P.
Downingic, the well-known Wenlock and Ludlow form.

The most common shells are, of course, Brachiopoda, as in all
these muddy sediments. Lingula Lewisti and L. Symondsi (MS.)
are plentiful; Atrypa, four species of Strophomena (of large size),
Discina, Crama, three species of Spircfer, four species of Orthis, six or
seven of Lhynchonella, just as in the Wenlock limestone: Pentamerus
linguifer and P. rotundus are the most plentiful of all; the latter
we have hitherto thought a rare species.

Of the other bivalve shells there are Cardiola, Mytilus, Pterinea,
Avicula, and Nucula. Avicule, of two or three species, are the most
common.

Spiral shells are not so plentiful. Huomphalus and Cyclonema are
rare. Bellerophon is abundant: there are three species, including
the great B. dilatatus of the ‘ Silurian System.’

The Cephalopod genera Orthoceras, Intuites, and Phragmoceras
also are rare. Lastly there is [schadites, which I have lately found
to be a genus of the sponges !

Tt will be seen how much this list is ike one made from the Lower
Ludlow deposits; indeed, in a broad view of the Silurian system,
one would not readily separate the Lower Ludlow from the Wenlock
rocks.

I have no notes on the Wenlock limestone along this section ; nor
is it very well developed. I believe it is cut out in many places by
faults not entered yet in any map.

Of the Upper Ludlow Rock which les between the Malvern ridge
and Rilbury Camp, it is enough to say that it contains the common
species in the usual proportions. When we meet with Chonetes lata,
Orthonota amygdalina, Orthis lunata, Orthoceras bullatum, and the
spiral shells (Murchisoma, &c.) with their investing Coral (Steno-
pora), we may be sure that the rest of the Upper Ludlow fossils are
not far off; Serpulites longissimus, for instance, with a lace-like
Bryozoan on its surface, &c.

The Aymestry bands near Rilbury Camp are not characterized
by any very peculiar fossils, so far as I know. The Brachiopods are
the most common. Instead of the Spirifer plicatellus of the Wool-

162 PROCEEDINGS OF THE GHOLOGICAL SOCIETY. [Jan. 9,

hope beds, we have Sp. elevatus in abundance. Rhynchonella Wilsont
is very plentiful; so are Lingula Lewis, Atrypa reticularis, and
Strophomena Pecten. Pentamerus galeatus is frequent; but I have
not the common P. Knightii in my list.

Only a few Univalves and Trilobites are known in this locality.

But if the limestone is poor, the Lower Ludlow shale beneath it
is prolific indeed. When I was there, they were bringing up the
grey-blue shale full of large Avicule, of the size and shape of the
Pearl-oysters. There was Pleurorhynchus, nearly as large as the so-
called Cardium Hibernicum! Besides a host of ordinary Brachiopods
(the list of which would be only a repetition of those of the Wool-
hope shale) and a very few Corals and Trilobites *, there are here the
largest Univalves known in the Silurian rocks. Plewrotomarie of four
or five species, some as much as five inches long; of Hwomphalus
three species; very fine Bellerophons, and the common Pteropods ;
Orthoceras, of great size and of many species; and the genera Phrag-
moceras, Cyrtoceras, and Lituites.

The profusion of Cephalopods from these beds in Dr. Grindrod’s
fine collection is wonderful. Among them is a new genus, to be added
to the British list, which my friend Dr. A. Fritsch f recognized as
one of the familiar Bohemian forms. It looks like a Jatuites, and
would have passed for a new species of it; but there is a slight spi-
rality in the whorls (not so great, however, as in several Bohemian
species), which betrays it. It is really a subspiral form belonging to
the Nautilide, and analogous to the genus Helicoceras among the
Ammonite group. It is 8 or 9 inches in diameter !

I believe that the “ Ludlow Bone-bed”’ is not found in the Tunnel-
section. You find it a few miles to the north, at Brock Hill and
also at Hales End, overlam by the Downton Sandstone.

The plant which Dr. Hooker described {, and for which he now
proposes the characteristic name Pachytheca spherica, is the common
fossil in the sandstone, and is accompanied, as at Ludlow, by plant-
remains and fragments of Pterygotus.

Of the “ Passage-beds,” described by you in your former paper §,
I need not say much; but having seen this beautiful section in your
company, I may be permitted to observe that I quite agree with
your interpretation of it. The little group of olive-coloured shale and
grey sandstone in which the Fish-remains are found, is exceedingly
like that in the larger section of the same beds at Ludlow. Of the
Fish-remains one is identical—the Cephalaspis Murchisom, Egerton ;
the other is a new Auchenaspis, certainly distinct from the Ludlow
species. Your section shows just what is wanting at Ludlow—the
300 feet of red marls and sandstones which intervene between these
passage-beds and the Silurian rocks, and which definitely shut the
former up in the base of the Old Red Sandstone.

* In the fewness of Trilobites this shale differs materially from the Woolhope
shale before-mentioned.

t Keeper of the Royal Bohemian Museum, Prague—an excellent observer,
and an authority on European birds. We passed three weeks in the Silurian
region most pleasantly together.

t Quart. Journ. Geol. Soc. vol. ix. p. 12. § Lbid. vol. xvi. p. 193.

1861. ] HUXLEY—PTERASPIS DUNENSIS. 163

JANUARY 23, 1861.
William Weston, Esq., Birkenhead, was elected a Fellow.
The following communications were read :—

1. On the Grave and Boutpers of the PUNJAB.
By J. D. Suiruz, Esq., F.G.S.

[ Abstract. ]

In the Phimgota Valley (a continuation of the Great Kangra or Palum
Valley) the Drift consists of sand and shingle with boulders of gneiss,
schist, porphyry, and trap-rock, from 6 inches to 5 feet in diameter.
Some of the boulders, having a red vitreous glaze, occur in irregular
beds.

This moraine-like Drift lies on the Tertiary beds, which, here dip-
ping gently towards the plains, gradually become vertical, and are
succeeded by variegated compact sandstones, gradually mclining
away from the plains; next come various slates, at a high angle;
and gneissic rocks lie immediately over them.

2. On Preraspis Dunensis (Archeoteuthis Dunensis, Roemer). By
THomas H. Huxtey, F.R.S8.,Sec.G.8., Professor of Natural History,
Government School of Mines.

Tue fourth volume* of the ‘ Paleeontographica’ of Dunker and Von
Meyer (1856) contains a memoir on “ Palwoteuthis, a genus of
Naked Cephalopoda from the Devonian rocks of the Hifel,” by the
well-known paleontologist Dr. Ferd. Roemer. The fossil upon which
this genus is founded is described as an oval, convex, symmetrical,
shield-like body, marked by two diverging longitudinal elevations
or keels, and exhibiting on its surface a peculiar ornamentation,
consisting of curved parallel ridges, so fine that there are as many
as8or1l0toaline. All traces of any deeper layer than that which
exhibits these ridges had disappeared. In discussing the affinities
of this fossil, Dr. Roemer decides in favour of its being the internal
shell of a Naked Cephalopod, upon the grounds, first, of its general
form, and secondly, of the presence of the diverging keels, in both
of which respects he considers the fossil to resemble the internal
shell of a Sepia. And he adds: ‘“ Inasmuch as the fine superficial
sculpture is altogether peculiar and different from that of the cuttle-
bone, and since, further, the fact that the fossil exhibits such a struc-
ture only upon its surface leads one to suspect that it was nota thick
ossicle, but thin and horny like that of Zoligo, and since, finally,
its occurrence in so old a formation makes its generic identity with
the living genus improbable, it will be justifiable to consider the
fossil as the type of a new genus, although its clear definition can _

* Page 72, plate 13.

164 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Jan. 23,

only be rendered possible by the discovery of more perfect specimens,
and perhaps of other parts of the animal.” (p. 74.)

Dr. Roemer then remarks on the evidence thus furnished of the
occurrence of naked Cephalopoda at an earlier period than had
hitherto been supposed; and, in a note, he refers to Dr. Kner’s paper
on Cephalaspis Lloydii and C. Lewisii, disputing the conclusion at
which Kner had arrived, that these fossils are remains of Naked
Cephalopods, and affirming “ that the structure of the shell of these
disks is rather that of Crustacea, and that their whole external form
leads to the supposition that they are allied to such paleeozoic Crus-
tacea as Dithyrocaris or Pterygotus.” Carefully executed figures
accompany the memoir from which these citations are made.

In Leonhard and Bronn’s ‘ Jahrbuch’ for 1858, p. 55, Prof. Roemer
returns to this subject, in a short “ Notice of a second specimen of
Archcoteuthis* Dunensis, from the clay-slates of Wassenach, on the
Laacher-See,” in which specimen the internal structure of the shell
is preserved,

«The form and size of this specimen,” says Prof. Roemer, “agree
essentially with those of the first specimen. Like the latter, it is
imperfect, the lower end being absent. ‘The fossil is a coal-black,
brittle, horny substance, sharply defined against the slaty grey of
the matrix; the thickness of the layer which it forms is about 2rds of
a line, as can be distinctly seen by the transversely fractured circum-
ference. The sculpture of the surface is to be observed only over a
small space. Here it exhibits the same fine lines as the Daun spe-
cimen. For by far the greater part of its extent, the superficial
layer of the shell is destroyed, and the internal structure is revealed
so distinctly as to make this specimen particularly remarkable. — It
consists of small prismatic cells, disposed perpendicularly to the sur-
face of the shell. The transverse section of the cells is irregularly
hexagonal, or even polygonal; the diameter of the cells is such, that
three or four occur in the space of a line, whence the separate cells are
perfectly recognizable with the naked eye. The depth of the cells
is equal to about one-third of the thickness of the shell. The lower-
most layer of the shell appears not to take part in this coarsely
cellular structure, but to be much more compact.

“Tf this structure be compared with that of the shell of Sepa
officinalis, L., the close analogy of the two is obvious. Only, in the
living genus the cells are much finer and are disposed in numerous
thin layers one over the other, whilst in the fossil species but a
single such layer is discernible. In any case, this cellular structure
of the fossil shell indicates its affinity rather with Sepia than with
Loligo, as I had previously supposed.”

The specimen from Wassenach thus described has now passed into
the collection of the British Museum; and my friend Mr. Woodward
(who had already divined the precise nature of the so-called Paleo-
teuthis in a note to p. 417 of his ‘ Manual of the Mollusca’) having

* In Bronn and Roemer’s ‘Lethza Geognostica,’ vol. i. p. 520, the name

Paleoteuthis, having already been employed by D’Orbigny, is given up, and
Archeoteuthis substituted for it.

1861.] HUXLEY—PTERASPIS DUNENSIS. 165

called my attention to the specimen, without giving me any informa-
tion as to its previous history, I at once affirmed it to be a Pteraspis,
—hbeing led to this determination by the eminently characteristic
striation of the outer surface, combined with the no less peculiar
polygonal cells of the middle layer*. There is nothing like either
of these tissues in any Cephalopod or Crustacean with which I am ac-
quainted—the construction of the cuttle-bone being totally different ;
and they exist, in combination, in no animal structure which has yet
been described, except Pteraspis. In form, and in the presence of the
diverging ridges described by Prof. Roemer, the fossil perfectly agrees
with many of our English Péeraspides; and I have therefore no
hesitation in expressing the opinion that Archwoteuthis must disappear

Diagram of a restored Pteraspis.

a. Snout or rostrum, united with 6, the shield-like disk. c. The cornua of the
latter ; d. its median backward prolongation ; ¢. the median posterior spine into
which the last is produced. jf. Orbits or nasal apertures.

* T have carefully described these structures in my memoir ‘‘ On Cephalaspis
and Pteraspis,’ Quarterly Journal of the Geological Society, 1858, vol. xiv.

VOL, XVII.—PRART I, N

166 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

from the list of Dibranchiate Cephalopods, and consequently that the
paleontological history of this group cannot, at present, be traced
back further than the beginning of the Mesozoic epoch.

The distinction of species among the Pteraspides is a difficult
matter; and, pending Givestipations which I have been for a long
time making on this subject, I leave open the question whether
Prof. Roemer’s specimens are or are not types of a new species,
which, in the latter case, must be termed Pteraspis Dunensis.

/In conclusion, I may remark that, as I have already pointed out
elsewhere (British Association Reports, 1858), the test of Pteraspis,
as commonly met with, consists of only a part of the cephalic shield
of that singular fish, the whole shield being not a little similar to
that of Cephalaspis. In Pteraspis rostratus, for example, the entire
shield has the form indicated by the subjoined outlines, of which A
represents a dorsal, and B a lateral view. It consists of a cephalic
rostrum (#), more or less elongated and pointed according to the
species, passing posteriorly into the broad shield (6), which (as
the dotted lines indicate) is commonly found broken off and alone.
When perfect, this is produced laterally and posteriorly mto two
cornua (¢), and in the middle line behind passes into a broad
prolongation (d@), which gives rise interiorly to a long, curved, and
backwardly produced spine (¢). Upon each side of the test, where
the rostrum joins the rest of the shield, there is a round well-
defined aperture (f), which may be either the orbit or the nasal
aperture.

It is not easy to find an exact parallel for such a cephalic covering
as this among existing fishes. Loricaria, Tetrodon naritus, Acipenser,
and Spatularia seem to present the nearest analogies,—the two
former being much more remote than the two latter. In fact,1f the
bony cephalic shield of the Acipenseroid fishes were ossified in one
piece, it would very closely resemble that of both Cephalaspis and
Pteraspis, and would hardly differ more from either than the two
from one another.

3. On the “ Cnark-rock,” the Topmost Bed of the Lowrr Cmax, in
Brrxsuree, Oxrorpsuire, Buckrnenamsuree, gc. By WitttAm
Wuitarer, B.A., F. G.S., of the Geological Survey of Great
Britain.

Tue bed to which I have elsewhere* given the name of “ Chalk-
rock,” I believe to form the division between the Upper and Lower
Chalk, and to be the topmost bed of the latter. I have described it
as “hard blocky chalk, jointed perpendicularly to the plane of bedding
with lines of irregularly shaped, hard, calcareo-phosphatie nodules,
which are green outside, but cream- coloured within.” It breaks
with an even fracture, rings when struck with the hammer, and is
of a pale cream-colour (the nodules being darker than the rest).

* Catalogue of Rock-Specimens in the Museum of Practical Geology, 2nd
Bricon, p- 596.

1861.] WHITAKER—CHALK-ROCK OF BERKS, ETC. 167

For some time I thought that this bed had escaped the notice of
geologists ; but Mr. Prestwich tells me that he has long known of it.
Tt has also been noticed by Mr. Evans, of Hemel Hempstead, and
Mr. W. Cunnington, of Devizes. However, I believe that no account
of it has yet been published, with the exception of the short de-
scription above referred to.

My own observations have been confined to the counties of Wilts, -
Berks, Oxon, Bucks, and Herts—that is, to the northern side of the |
western part of the London Basin,—in which area I found that the
Chalk-rock reaches its greatest thickness to the west, gradually thin-
ning eastwards.

I have found but few fossils in the Chalk-rock; but Mr. Evans
most kindly sent those that he had collected (near Boxmoor) to the
Museum of Practical Geology. They have been determined by
Mr. Etheridge, and they make up the greater part of the following
list :—

Fossils of the “ Chalk-rock.”

Baculites. Spondylus latus.
Nautilus. Sp. spinosus.
Rhyncholites (of Nautilus).
Turrilites. Rhynchonella Mantelliana.
Terebratula biplicata.
Trochus ? T. semiglobosuw.
Turbo ? ==
Parasmilia.
Tnoceramus.
Pachymya ? Ventriculites.

In Wiltshire I saw only one section of the Chalk-rock, not having
time to search for others; this, however, showed a far greater thickness
of it than Ihave elsewhere seen. It is in a cutting on the turnpike-
road leading up the chalk-escarpment that forms the northern side
of the Pewsey Valley, nearly four miles 8.8. W. of Marlborough. The
Chalk-rock is cut into near the top of the hill; and the following
alternations may be seen in it :—

ft. in.
Nodules, with a little cherty flint at the top
LAN DAR US Scena nude cote eictae Mam eEC clay tris about 3 3
arderockyachalicny ss cctv hase acc ner
INOdUIES Hees eae loan eior oy Petr earn narc each } 2 3
j 5 Geavra bite] vai Ue ee Opn I ces eu lela ae le 22
INOd Wiles es erer gs hee Pc eet ee Re. 160,
Marcle bie comers cee se ae8 Oona tari ee meiineget ote Ya 24
Mil eLOLENOMULES a zyac eke ce elemese ete ee c i
TB tan) (lave ex oa em TO eG emi atl re sae a
INO GUESS Bem eA tage Gait Raha ce eee teee
itland prockayachealllkarm rests ae ven suis 2) e sie) sore aN
Mar lyascambrerratie etaan erase sds tie ss 16> 4
Ia dae lve lke geen er Mac ae Gide, age cis 6s
INOUE Siimes em amONE NN Us ue ease Sou Fe ev Oia ee
11 4

168 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

As the beds below the last line of nodules were hidden by fallen
rubbish, I could not see the full thickness of the “rock.” The beds
of nodules are two or three inches thick.

Working eastwards, the next place at which I have seen the
Chalk-rock is in the neighbourhood of East Llsley, in Berkshire,
where, indeed, I first noticed it. Here its thickness is not much over
4 feet. ;

About half-way between Pangbourn and Bassildon, in a large pit
on the Oxfordshire bank of the Thames, it is seen to be about 6 feet
thick; and in the neighbourhood of Henley-on-Thames it is about
4 feet. At this last place, the Chalk-rock and the Lower Chalk occur
as an inlier, being surrounded on all sides by Upper Chalk. There are
three good sections on the northern side of the Thames between Henley
and Medmenham. In these, as well as in the section above Pang-
bourn, its position in the Chalkis well shown. It forms an exact line
of division between the Upper Chalk (with flints) and the LowerChalk
(without flints),—there being generally a bed of flints lying on its
upper surface, whilst there are none either in or below it, with the
following exception, which does not in any way disprove the rule.
In a chalk-pit just above Greenland Lodge, near Henley, there is a
section across a small fault, from which, below the Chalk-rock,
proceed two. highly inclined fissures, some feet in length, but not
more than a quarter of an inch broad; each of them is filled with
a line of flint, which must clearly have been deposited from some
siliceous solution that found a channel down the fissures, and
which must therefore be of later date than those fissures. These
two lines of flint have no relation to the beds of flints in the chalk
above the “rock,” but are inclined’ at a high angle to the line of
bedding.

Still working eastwards, the Chalk-rock may be occasionally seen
along the chalk-escarpment, at no great distance from the top, and
also on the flanks of the main valleys running at right angles to the
strike of the Chalk (and differing from the lesser valleys, which are
dry, in containing streams).

As the dip of the Chalk is not much greater than the fall of these
valleys, the Chalk-rock does not disappear along them for many
miles inland from the escarpment. Thus, along the Loudwater
Valley it occurs as far south as Wycombe Marsh; in the Misbourne
Valley it reaches to a point a little below Amersham; along the
Chess Valley, to nearly three miles below Chesham; and in the
Berkhampstead Valley to some spot between Boxmoor and King’s
Langley.

Near High Wycombe, and to the east of that town, the Chalk-rock
loses its hitherto well-marked jointing, and breaks up into compara-
tively small pieces. In the neighbourhood of Wendover, Amersham,
and Berkhampstead, its thickness has dwindled down to 2 or 12 feet ;
but on the hills to the south-east of the first place there are two beds
of it, separated by a few feet of chalk.

The last section of the Chalk-rock that I saw was in a pit near the
Boxmoor Railway-station, where for the first time I noticed beds of

1861. WHITAKER—CHALK-ROCK OF BERKS, ETC. 169
i}

flints below the rock. Of these I saw but two; and in each the flint-
nodules were widely separated: it is possible that here also there
may be a second bed of the “‘rock” lower down. Besides the sections
that I saw, I also often heard of the occurrence of this bed in well-
sinking. Where it is thick, the well-sinkers are obliged to blast it,
on account of its hardness.

Where there are good clear sections, as near Henley, its upper
boundary will be seen to be sharply defined, the lower one not; so
that I should take it to belong to the Lower rather than to the Upper
Chalk. The few fossils that have been found in it bear out this
view.

In the parts of the chalk-country of Surrey and Kent known to
me, I have not noticed the Chalk-rock; but my friend and colleague
Mr. Drew tells me that he has seen, in the former county, a bed
that seems to be like the Chalk-rock of Bucks, Berks, d&c., and in
the same position. It may be seen on the flank of the chalk-escarp-
ment in the large quarries near Guildford, and in others between
Dorking and Reigate (north of the word “ Betchworth ” on the
Ordnance Map), where it is about 25 feet thick; and also in the
valley along which the Caterham Braneh-Railway runs, at the
Rose and Crown, about four miles north of the escarpment. The
following section taken at this last place has been given me by Mr.
Drew :—

HVECONSLIACted) Chal ka auch actin stakes oni aranan 4 or 5 ft.
Ghrallkcryatblatlinitsiek ie, esta sivas, heat, eos rere ei aii about 25 ,,
Chalk with nodular structure and a few seattered

tims) (Chalknocls 2) 5 sey catia tect eye cys Sale DE ined
Chalk awa thou Hints. ccuencmere cop erccu cigteencrs Pa easy ays

From the above, it is clear that the bed is very thick about
here*.

From the account of the chalk-cliffs near Dover, given by Mr. W.
Phillips, in the ‘Transactions’ of the Societyt, I cannot clearly
make out its presence there. If it be present, it must be in great
thickness.

The “ Chalk-rock,’”’ should it prove to be the topmost bed of the
Lower Chalk, as it is in the counties of Berks, Oxon, and Bucks, must
have some influence on our notions as to the extent of country taken
up by that division of the Chalk. In the above-named counties the
Lower Chalk forms nearly the whole of the great escarpment, not
being covered by the Chalk-with-flints until within a short distance
from the top, except at the highest points of the range; runs along
the main valleys for eight, ten, or twelve miles from the escarpment;
and, according to well-sections in brick-yards, is but from 40 to 80

* Mr. Drew has lately revisited the chalk-country between Farnham and
Guildford, and he tells me that the Chalk-rock is about 25 feet thick in that
neighbourhood also.

t Ist Series, vol. v. p. 16, &e.

170 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Jan. 23,

feet below the surface for a considerable distance from its outcrop*.
As in the counties in question the Upper Chalk is not far short of 300
feet in thickness, and sometimes quite that, it is clear that the top-
most beds of the Chalk do not generally occur either on or near the
escarpment, but that they have been denuded. The Chalk-rock will
serve as a datum for the measurement of the extent of this denu-
dation.

There are two more points that may be noticed in connexion with
the Chalk-rock. To the north and north-west of Marlborough, the
Upper Chalk has an escarpment of its own, quite distinct and separate,
and often at a considerable distance, from that of the Lower Chalk, as
noticed by Mr. Aveliney. May not this be owing to the Chalk-rock
being there very thick, as there is every reason to suppose is the case ?
Further eastwards, where the Chalk-rock is thinner, the two esearp-
ments generally merge into one.

In parts of the South of England there are flints from the top to
the bottom of the Chalk. Ido not know whether it is supposed that
this flint-bearing Chalk represents both the Upper and Lower Chalk of
other parts, or the former only. The occurrence of the Chalk-rock
might set at rest the question whether the Upper Chalk only is there
present, or whether the Lower Chalk is flint-bearing. The former
case would imply an overlap between the Upper and Lower Chalk.

Posrscript.—Since this paper was read, Mr. Prestwich has told me
that he has seen the bed in question on the top of the chalk-hills
between Calne and Marlborough Downs ; that it was found in a well
at Harpenden, near St. Albans; that it has been noticed by Mr.
Bensted and others on Kit’s Cotty Hill, near Maidstone (where it is
but 2 or 3 feet thick); and that the nodules in it have been found to
contain ten per cent. of phosphates,

A more detailed account of the sections of the Chalk-rock in
Oxfordshire and Berkshire will be given in a memoir (shortly to be
published) illustrating Sheet 13 of the Map of the Geological Survey ;
and those in Buckinghamshire will be noticed in a memoir (now in
progress) to illustrate Sheet 7.

* T find that Mr. Godwin-Austen has noticed the extent to which the chalk-
escarpment of Berkshire consists of Lower Chalk. He says, ‘the highest point,
Uffington Camp, appears to rise no higher im the series than the Chalk-without-
flints.”” (Quart. Journ. Geol. Soc. vol. vi. p. 461.)

+t See Memoir illustrating Sheet 34 of the Map of the Geological Survey of
Great Britain, p. 37.

1861.]

MURCHISON AND GEIKIE—HIGHLANDS,

7a

Frsruary 6, 1861.

Willham Rutherford Ancram, Esq., 75 Inverness Terrace, Ken-
sington Gardens, and Thomas William Jeffock, Esq., C.E., Woodside,

Sheffield, were elected Fellows.

The following communication was read :—

On the AurereD Rocks of the Western Istanps oF Scornann, and

the NortTH-WESTERN and Crentrat HIcGiHLANDs.

By Sir Roperick

J. Mourcuison, D.C.L., V.P.G.S., F.R.S., &c., and ARcHIBALD

Grixiz, Esq., F.R.S.E., F.G.S.

ConTENTS.

Introduction.

§ I. Laurentian Gneiss of the Hebri-
des and North-western Highlands.
1. Lewis and Harris. | Lewis.
2. Cambrian Conglomerate of the
3. Laurentian Gneiss of the main-

land.

§ II. Cambrian Sandstone and Con-
glomerate of Ross-shire.

§ III. Succession of Lower Silurian
Quartz-rocks, Limestones, and
Schists.

1. Sutherland to the Isle of Skye.
Craig-an-Knochan.
Drumdrynie. Strath Kennort.
Loch Auchall. Loch Broom.

From Loch Broom to Loch Maree.

Loch Maree.
Loch Maree to Loch Torridon.

The “ Grey Heads.” Loch Carron.
Skye.

Loch-alsh. Loch Duich.
2. Structure of the country between
the Atlantic and the Line of the
Great Glen or Caledonian Canal.
Loch Broom to Contin.
Loch Hourn by Loch Quoich to
the Caledonian Canal.
Arisaig to Banavie.

3. Repetition of the Lower Silurian
Quartz-rocks, Limestones, and
Schists east of the Line of the
Great Glen.

Line of Great Glen or Caledonian
Canal. Islay and Jura.

Prolongation of the Islay and Jura
Rocks up Linnhe Loch.

Eastern shore of Linnhe Loch.

Glen Spean. Loch Leven.

Glen Coe.

The Breadalbane Deer-Forest.

Black Mount by Glen Orchy to
Loch Awe.

Black Mount to Tyndrum.

Tyndrum to Loch Tay.

Loch Tay.

Loch Tay to Glen Lyon.

Taymouth to Loch Rannoch and
Dalnacardoch.

Dalnacardoch to Blair.

Blair-Athol and Glen Tilt.

Blair to Dunkeld.

Spittal of Glenshee to Dunkeld.

Eastern Flanks of the Grampians.

§ IV. Conclusion.
§ V. Appendix.

Introduction.—In former memoirs upon the crystalline rocks of

the north of Scotland, read before this Society, it was shown by one
of us, that in the county of Sutherland, in addition to the existence
of a fundamental gneiss and an unconformably superposed Cambrian
sandstone, there is a conformable ascending series, from certain
Lower Silurian quartz-rocks and limestones, up into a group of mi-
caceous and gneissose schists. It was also pointed out, in a general
sketch-map of the Highlands*, that the order thus observable in

* Tn perusing this Memoir, the reader is referred to the geological sketch-map of
the Highlands previously published in Quart. Journ. Geol. Soc. vol. xv. pl. 12. That
map, suggestive of that geological order in the Southern Highlands which we have
since worked out, will speedily be followed by a general sketch-map of all Scotland,
with illustrative coloured sections, in which the correlation of the stratified rocks
of the Highlands with those of much less altered characters in theSouth of Scotland,
and containing Silurian remains, will be for the first time explained by ourselves.

172 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

the north-western regions of Scotland probably extended south-
wards across the mountainous tracts to the south of the Caledonian
Canal. But this application of the classification of the rocks of the
north-west was based on general observations only of earlier years;
and a more exact survey was culled for before it could be held as
proved that the great mass of the Scottish Highlands displayed the
same order of succession as had been demonstrated to exist im the
north-western tracts.

It was also necessary to trace the development of the Sutherland-
shire series to the south-west, through Ross-shire, so as to complete
the base-line from which the rest of the Highlands should be worked
out in detail.

For this purpose we devoted two months of the last summer to an
examination of the Ross-shire district and the region southwards to
the Highland border, including the islands of Lewis, Skye, Islay, and
Jura. The results of this survey, completely confirming our previous
views, are laid before the Society in the present memoir.

I. Rane or tHe LAURENTIAN oR OtpER GNEISS IN THE HEBRIDES
AND NorrH-Westrern HigHuanps.

Lewis and Harris.—As announced in previous memoirs, the
greatest spread of the Older or Laurentian Gneiss is seen in the Long
Island of the Hebrides, by mnch the larger portion of which is called
“« the Lewis*,” the lesser or southern part being “ the Harris.”

In both these tracts the mineralogical character of this older
gneiss, and its numerous contortions, have been so well described by
Macculloch, that little remains to be said on those heads by others.
That author has, however, omitted to state that the usual and
dominant direction of the strata is transverse to the elongated form
of this island ; for, whilst the geographical axis of the whole, as seen
in any map, is from N.N.E. to 8.8. W., the normal strike of the beds
of gneiss is from $.E. to N.W., or across the island. The traveller
who has not much time at his disposal may convince himself of this
fact in a few hours by examining the rocks which rise up to the
west of the Port of Stornoway. If he should have sailed from the .
opposite mainland, and have there observed that on the shores of
Lochs Maree, Gairloch, and Torridon the Laurentian gneiss has a
persistent strike from N.W. to 8.E., with dips to the N.E. and 8.W.,
he will find precisely the same phenomena in the Lewis.

Whether he examines the various points of rock—so well exposed
in the pleasure-grounds of Stornoway Castle, and particularly those
which have been cut through by Sir James Matheson on the banks
of the torrential river Creed, or the sea-cliffs of the headlands on
the east—or should cross the peat-covered moors, to the western
shores and the interior, to Morsgail or to Soval, or even should
extend his researches into the Harris beyond Athline,—he every-
where meets with the same phenomenon of a prevalent strike from

* Pronounced ‘ Lews.”

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 173

N.W. to S.E. with countless undulations, and decided inclinations at
all angles, both to the N.E. and 8.W.

In saying that the strike is from N.W. to 8.E., it must be added
that this direction sometimes varies slightly to the N. and S. of
N.W.and8.E.; but the normal strike is precisely that which prevails
also in rocks of the same mineral character on the western shores of
the mainland in Ross-shire and Sutherland.

As before shown*, the strike of this old or bottom gneiss is there-
fore at right angles, or nearly so, to the N.E. and 8.W. direction
of all the superjacent crystalline rocks of the mainland, including
the quartz-rocks and limestones, and .all the overlying formations.
In no part of the Lewis is this dominant strike better exhibited than
in the hilly deer-forest of Sir James Matheson at Morsgail. ‘There,
and adjacent to the shooting-lodge, the gneiss is admirably exposed
in several openings, and consists of infinite alternations of highly-
inclined dark hornblendic and whitish quartzose laminze, which beds,
as exposed on the sides of a burn, are rolled over and over into
numerous contortions, with dips both to the 8.W. and N.K. ‘These
strata are every here and there diversified with protrusions of highly
erystalline hornblende-rock, in parts a greenstone, which rise in large
round masses, or are distributed in geodes and layers. The abun-
dance of iron in this rock occasions the decomposition of its surface
into holes and irregular cavities; and numerous masses so honey-
combed strew the edges of Loch Morsgail.

In the hills of Scalaval, all the gneiss, whether quartzose, horn-
blendic, or felspathic (more rarely micaceous), has again the direc-
tion from N.W. to 8.E., or to points slightly deviating therefrom.
The same is seen in the mountainous masses along the shores of
Loch Langabat, where the N.E. or 8.W. inclination of the beds is
strongly contrasted with the great transverse fissure occupied by that
long sheet of fresh water, which, on the contrary, is parallel to the
geographical axis, 7. ¢. N.E.-S.W., and therefore nearly at right
angles to the strike of the ancient strata of gneiss. In short, the
phenomenon of the trend of the hills and valleys on the actual con-
figuration of the surface being transverse to the original direction of
_ the strata is as strikingly exemplified in the Lewis and Harris as it is
in the Harz and other masses of rock on the continent of Europe7y.

Such contrasts between the original direction of the layers of
deposit and the geographical outline of the islands are also strikingly
displayed where the low and moss-covered hills of the Lewis rise into
the mountains of Harris.

Passing from Loch Seaforth into the rocky glens of Vickadell and
Scaladell, and under the frowning steeps of Craig Arig, the Clishan,
Moolan Gorran, and Scorse Scaladell, the highly crystalline gneiss
(here quartzose and grey) still ranges from N.W. to 8.E., and dips
either to the 8.W. or N.E.+

* Quart. Journ. Geol. Soc. vol. xvi. p. 216.

+ See Quart. Journ. Geol. Soc. vol. xi. p. 449, and ‘Siluria,’ 1859, p. 414.

t These glens of Harris, radiating from lofty and steep mountains, afford
splendid evidences of glacial action, their mouths and flanks being studded with

174 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

In numerous places the strata are strikingly interfered with by
intrusions of granite, as well as by hornblende-rock and greenstone.
In one tract only, however, that fell under our observation does gra-
nite occupy so considerable a surface as to be entitled to a place in
our forthcoming sketch-map of Scotland,—a feature unnoticed by
Macculloch and other geologists. This mass of granite comes out
at Dalbeg, on the west coast of Lewis. There, whilst the hills of
Barayas range in geographical outline from N.E. to8.W., the granitic
ridge is protruded from them to the coast on the north-west, and is
thus shown to conform in its direction to that of the main masses
of the ancient gneiss. This granite is coarse-grained and of various
colours (though the prevailing tint is red), and, containing felspar,
quartz, and mica, is entirely free from hornblende. As veins of this
granite traverse the gneissose rocks, it is evidently of later origin
than the deposition of the gneiss.

Besides the usual varieties of gneiss, whether consisting of layers,
of quartz and felspar with mica or with hornblende, white hyaline
or flinty quartz is occasionally seen in the form of layers of both pink
and white colours, sometimes presenting the appearance of having
been injected amid the layers of gneiss, in the same manner as
the numerous granitic veins. In some places the laminated and
bedded gneiss has undergone great decomposition, as at Garrabost,
in the promontory of Eye. There, near the entrance of the Chemical
Works * under the direction of Mr. Paul, the gneiss, consisting of
fine layers of quartz, felspar, and mica, has been so affected by
atmospheric influences as to exhibit the following appearances.
The felspar having decomposed and passed into heaps of clay, the
quartz-grains and the flakes of mica remain in the form of a frame-
work which might pass for an incipient band of soft ordinary mica-
ceous sandstone formed on the shore of the present sea. Again, the
felspar of the old gneiss contains a considerable admixture of lime,
and hence it affords, on decomposing, not merely good clay, but
much carbonate of lime in solution. Thus detached fragments of the
overlying conglomerate, of which we are about to speak as seen on
either side of the bay of Loch Tua, over which the water trickles
down from the decomposing gneiss to the shore, as well as the
pebbles and shells of the present bay, are bound together on the
slopes of the cliffs and on the sea-shore by the cementing carbonate
of lime, and form a hard calcareous grit and conglomerate. Before
we quit the consideration of this fundamental British rock, as seen in
the outer Hebrides, we would beg our readers to consult the various
chapters of Dr. Macculloch in which he dwells upon the dull and
monotonous character of the gneiss in all this range of islands, as con-
trasted with the descriptions of the same author of his so-called gneiss
of interior portions of the mainland. For, although he grouped various
and dissimilar rocks in the family of gneiss, and gave no proofs of

stupendous erratic blocks. The hills of the Lewis are too low to have been the
seats of glaciers; and on that northern portion of the island erratics are scarcely
to be discovered.

* For the distillation of bitumen from peat.

~

1861.] MURCHISON AND GEIKIE—HIGHLANDS, 175

their true succession, he had, even in his day, so faithfully delineated
the essential mineralogical distinctions between the gneiss of the
Western Isles and that of large tracts of the mainland on the east, as
to prepare the way for those who, like ourselves, have worked out the
proofs of a clear order of superposition. Combining these proofs of
succession with the manifest distinction in the lithological structure
of the two classes of rock, we are of opinion that no geologist can
confound the Laurentian or fundamental gneiss with the so-called
eneiss of the superior crystalline schists, which, instead of being a
massive hornblendic and granitoid rock like the first-formed, is, on the
whole, a flag-like, micaceous, and quartzose deposit of very different
characters.

Although we have not, like Macculloch, traced the persistence of
this same Hebridian or Laurentian gneiss through all the isles where
it abounds, we have observed it in the Isles of Rona and Raasay. It
forms the whole of the former island, and the northern end of the
latter at Castle Brochel in Raasay; it is overlain by Cambrian shales
and sandstones, which, towards the south end of the island, are re-
placed by coarse conglomerates, well seen in the watercourses south
of the road from Raasay House* to the eastern shore, as well as
along the cliffs of the opposite Island of Scalpar.

Cambrian Conglomerate of the Lewis.—With the exception of
superficial accumulations of sand, clay, or pebbles, the island of
Lewis offers nowhere any deposit overlying the ancient gneiss, except
an old conglomerate composed exclusively of fragments of that rock,
associated with a few sandy layers. These beds are exhibited at in-
tervals on both sides of the Bay of Loch Tua. They are made up of
pebbles of the older gneiss, varying from the smallest size to boulders
larger than any among the Cambrian rocks of the mainland: their
chocolate-red colour, precisely that of the sandstone strata of Suther-
land and Ross, is probably due to the extensive decomposition of
the iron of the hornblendic masses which prevail in the subjacent
gneiss.

As this conglomerate is unknown in the Lewis, except upon the
headlands and bays east of Stornoway +, where it is exactly opposite
to the Cambrian conglomerates and sandstones of the mainland of
_ Ross-shire, which also are formed exclusively out of the subjacent
bottom-gneiss, and dip away to the west, as if passing to the Lewis,

* Mr. Geikie has explored and mapped the geology of Raasay, with reference
especially to its Oolitic strata, and hopes soon to be able to lay the results before
the Society.

Tt In a new sketch-map of Scotland, now in course of preparation, we have
represented the Isles of Tiree, Coll, and Iona as composed essentially of Lauren-
tian gneiss, not only because they are identified with the gneiss of the Long
Island by the minute description of Macculloch, but also from the independent
testimony of the Duke of Argyll, who lately visited his property in Tiree.
Thoroughly well acquainted with the character of the so-called gneiss of Argyll-
shire, where granites and intrusive rocks equally abound as in the ‘Hebrides, his
Grace so recognized the striking lithological distinction between the two classes
of rock, that he declared to us that no such gneiss as that of Tiree exists on the
mainland.

t The Lighthouse and part of Stornoway stand on this conglomerate.

176 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

there can be little doubt, in our opinion, that the Lewisian beds
formed the western or shore-side of an extensive trough of a deposit
of the same age, the central portions of which are covered by the
waters of the broad channel of the Minch.

On the mainland, indeed, there are decisive proofs that these
sandstones and conglomerates are of Cambrian age, because they are
clearly surmounted, as shown in previous memoirs, by strata con-
taining Lower Silurian fossils. In the Lewis, however, where there is
no upward sequence, the inference that they are of the same remote
age must rest upon the fact of their bemg made up exclusively of the
Laurentian gneiss, and on the appearance they present of having been
a portion of the same great range of red and chocolate-coloured
sandstones which occupy the opposite headlands of Ross and Suther-
land. At the same time it is right to state that the sandy beds in-
tercalated in the conglomerates of the Stornoway headlands are so
infinitely less coherent than the red sandstone of the mainland (for
the thin courses of sand in the Lewisian beds are rarely in the form
of solid stone, but have rather a soft marly character) that some
doubt must always remain as to the true age of these insulated de-
posits. It is the more essential to enter this caveat, because there are
red conglomerates at various places along the west coast of Scotland
(as, for example, at Oban), the ages of which are also incapable of
rigorous demonstration, from the absence of any overlying deposits.

The conglomerate of the Lewis is cut through by dykes of green-
stone, which have a direction from N, by W. to 8. by E., and are well
exposed on the northern face of the headland of the Eye. Contain-
ing some olivine, these dykes of greenstone have produced a marked
effect on the conglomerate through which they cut, as seen on the
sides of the cliffs. Flanked on either side by a thin “ Sahlband” of
Lydian stone which separates the greenstone from the conglome-
rate, the latter is for a yard of a whitish colour,—the red colour of
the rock, as due to the presence of iron, having been driven off.

Laurentian Gneiss of the Mainland in Ross-shire.—Deseriptions
have previously been given of the character of the older gneiss of
Sutherland, where it usually forms low headlands on the sides of
deep bays, and is unconformably surmounted by mountainous masses
of Cambrian Sandstone. The same rocks, extending southwards
along the western shore, expand largely in Ross-shire, as exhibited in
Gairloch and on the sides of Loch Torridon, as well as on the eastern
side of the long freshwater Loch Maree. On the right bank of Loch
Maree this gneiss contains both limestone and ironstone, which occur
in bands regularly interstratified, and which have the normal strike
of these ancient beds, as in the outer Hebrides. This strike from
N.W. to S.E. is therefore parallel to the great depression occupied
by the water of Loch Maree. In no portion of the North-western
Highlands is there a tract which more completely exhibits the en-
tire independence of this Laurentian gneiss of all those overlying
deposits, also termed gneiss, with which Prof. Nicol has recently
sought to identify it, both in his Geological Map of Scotland and
in his memoir read before the Geological Society. We therefore

1861.] MURCHISON AND GEIKIE—-HIGHLANDS. G7

eall special attention, not only to the N.W. strike of the beds of this
fundamental rock, as contrasted with the north-easterly strike of the
eastern rocks, but also to the marked distinctions in lithological com-
position between it and any of the overlying masses.

The older gneiss which ranges along the north-eastern side of
Loch Maree, and rises in some places to several hundred feet above
the water, 1s unmistakeably the same hard, massive, and highly
crystalline rock as elsewhere in the outer Hebrides and the coast of
Sutherland. At several places it exhibits subordinate layers of fine
schistose limestone, which above the House of Letter-Ewe is encased
in dark-grey gneiss (fig. 1), occasionally schistose, with white quartz-

Fig. 1.—Section across Loch Maree at Letter-Ewe.
S.W. N.E.

COTS ss:

Ls Toe

Loch Maree.

a. Gneiss. a*, Schistose limestone.
b. Cambrian sandstone and conglomerate.
c. Quartz-rock.

veins. This limestone, which has been quarried by the proprietor on
both sides of the torrent Fuolish, is for the most part a whitish or
cream-coloured, scaly, fracturing rock, and, though here and there
mixed with earthy greenish schist and gneiss, it is in parts a bril-
liant snow-white saccharoid marble. Whether, therefore, we look
to its composition, or to that of the enveloping gneiss, this limestone
is as distinct as possible from the dull grey-and-white limestone,
which, subordinate to the quartz-rock and overlying series of strata,
has also a totally discordant direction. The one rock must therefore
have been formed long ages before the other.

In the sequel we will endeavour to show, when explaining the
details of another section, that it is physically impossible that this
Laurentian gneiss of Loch Maree should, by any great upheaval, be
so placed as to lie conformably upon Lower Silurian limestone and
quartz-rock to the west of Kinloch Ewe. In the mean time we
would point to the geological map of Professor Nicol, to indicate a
serious erratum as to the direction of this limestone, which occurs in
the gneiss of Loch Maree. It is therein represented as directed from
N.E. to 8.W., and therefore as passing across to the 8.W. side of the
loch*, If this were correct, some persons, who have not visited the

* Prof. Nicol has here, and in many other portions of his map, followed
Macculloch.

178 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

tract, might be led to believe that this lower gneiss, being parallel
to the gneiss on the 8.E., was truly part and parcel of the same
series of deposits as the rocks on the 8.H.; for im that case they
would only have to imagine the intervention of a stupendous fault.
But the plain fact entirely overthrows this hypothesis. The older
or gneissose limestone trends rectangularly to the direction which has
been assigned to it, and hence it cannot (being a true bed) traverse
the loch as represented. In fact, there is no trace of limestone on
the left or 8.W. bank of Loch Maree, though, at some miles distant,
in Gairloch, and, again, subordinate to the north-westerly strike of
the Laurentian gneiss, another thin course of limestone has been
detected, and partially worked. In short, between Loch Maree and
the sea-board at Gairloch, wherever the fundamental gneiss is un-
covered in low masses beneath the superjacent masses of Cambrian
sandstone (the highly-inclined strata being admirably exposed in
the gorge wherein the River Kerry forms the picturesque Falls of
Andresy), the persistence of the N.W. strike is clearly maintained.

Again, near Shieldag, and at the headlands on either side of the
mouth of the maritime Loch Torridon, as seen at the Point of Grabeg,
and extending up the loch westwards, the Laurentian gneiss has the
same north-westerly strike as in Loch Maree and Gairloch, in Suther-
land, and in the Lewis, and is seen dipping sharply to the N.E.
wherever its eroded edges thin off into low hummocks under the stu-
pendous and mountainous masses of the Cambrian sandstone forming
the rugged overhanging cliffs on both shores of Loch Torridon.

In this district the underlying massive gneiss is perforated by
numberless intrusions of granite, as in the fiords of Sutherland, and
is in itself undistinguishable from the rocks of the same age which
range from Cape Wrath to Loch Inver*. It is therefore, we repeat,
most easily distinguished by its general aspect and structure from
the overlying flag-lke rocks with which it has been confounded.

II. Camsprran Sanpstone anp ConeéLoMERATE.

In former memoirs these rocks, particularly as they occur in
Sutherland, have been so fully described, whether, as formerly,
under the misnomer of Old Red Sandstone, subsequently by Pro-
fessor Nicol as simply Red Sandstone, or by one of us as Cambrian,
that on this occasion we need only advert to them in their prolon-
gation through Ross-shire from the north of Loch Broom on the
N.N.E. to Applecross on the $.8.W.

In this tract these rocks range from about sixty miles in length,
and over an average width of not less than twenty miles, and form
clusters of mountains varying from 1500 to 3500 feet above the sea,
their lowest beds being seen in numerous places to repose on the
Laurentian or fundamental gneiss. The promontories on both sides
of the marine Bay of Gairloch, as well as the noble mountains of
Applecross, consist of slightly inclined masses of this chocolate-
coloured sandstone, which there dip very gently seawards from off
the older gneiss, or to the W.N.W. In following these same rocks

* Quart. Journ. Geol. Soe. vol. xv. p. 361; and vol. xvi. p. 218.

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 179

towards the interior of Ross-shire, their lower beds, particularly on
both sides of Loch Maree, either consist of conglomerates made up
exclusively of the gneiss on which they rest, including much white
quartz and felspar, or they are very coarse grits, which pass upwards
into the fine siliceous chocolate-coloured sandstone. This junction
of the lowest beds of the Cambrian is well exposed on the N.E. side
of Loch Maree, on the sides of the Haasach Stream, and particularly
at the base of the lofty mountain Sleugach, which is essentially a
Cambrian rock. There the fundamental gneiss, in low headlands,
dips 8.W. at 70°, and the overlying sandstone, at 10° to 12°, to the
K. by N.

Again, on the opposite or western side of Loch Maree, where the red
and chocolate-coloured sandstone, covered by gorgeously rich thickets
of fern, heather, and grand old Scotch-firs, approaches the older gneiss
of Gairloch on which it rests, the basement-strata become first coarse
and gritty, and then form here and there pebbly conglomerates.

From the western shores of Loch Maree this Cambrian sandstone
rises into a noble, lofty group, some of the summits of which, being
capped by whitish Lower Silurian quartz-rock, have led the natives
to style these mountains “Ben Too leach,” or “ the Grey Heads.”
Looking from the hills east of Loch Maree to these mountains on
the west, which range from Ben Eay by Roostag to Ben Alligen,
on the south side of Loch Torridon, the spectator has within his
vision massive mountains, whose summits range from 3000 to 3500
feet above the sea. Now, all the strata of this mountain-group,
which cannot on the whole be estimated ds having a less thickness
than 7000 or 8000 feet, and which rest in unconformable positions
on the Laurentian gneiss, are on numerous summits capped by un-
conformable strata of quartz-rock with subordinate limestone. In
fact, the Cambrian strata undulate in such slightly inclined positions
as seldom to exceed 12° or 15°, whilst the subjacent gneiss and the
overlying quartz-rock are frequently highly inclined. These Cam-
brian rocks, whether inclining gently to the W.N.W. or to the
E.S.E., constitute therefore a thick series of intermediate strata,
which are quite unconformable both to the rocks beneath and to
those above them.

In striking contrast to these unconformities, we shall presently
point out that, along a frontier of many miles in length, the geolo-
gist has no sooner passed over the fundamental eneiss and the Cam-
brian sandstone, and marked the transgressive junction of these
rocks with each other and also with the overlying quartz-rock, than
he meets thenceforward, in all the great overlying crystalline masses,
with a perfect conformity of direction of all the strata to each other ;
and that (omitting a few spots where local dislocations have oc-
curred) there exists a perfect ascending order from the Lower Silurian
quartz-rocks and limestone into younger and higher masses of mica-
ceous, quartzose, and chloritic rocks (including occasionally a younger
gneiss), not merely in the North-western Highlands, but also in the
Southern Highlands, including the Isles of Islay and Jura, and the
counties of Inverness, Argyll, Perthshire, &c.

180 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

IIL. Succzsston or Lower Srivr1an Quartz-Rocks, LrwEstonus,
AND SCHISTS.

1. Sutherland to the Isle of Skye.

In a former paper, the succession of Lower Silurian quartz-rocks
and limestones upon Cambrian sandstones was traced to the southern
confines of the county of Sutherland. In the present memoir we
propose to take up the lines where they were then left, and trace
them southwards through Ross-shire into Skye.

Craig-an-Knochan.—The enormous escarpment of limestone that
ranges southward from Inchnadamff becomes less in its southward
progress, owing to a gradual thinning away of the calcareous strata.
The general succession, however, remains the same. These facts
are well shown at the watercourse which divides the counties of
Sutherland and Ross, where it pours over the cliff of Craig-an-
Knochan. This cliff, here from 60 to 100 feet high, is formed by
the escarpment of the limestone, and shows along the whole course
a clear section of the strata. The road which skirts its base runs
upon the white quartz-rock that stretches westward, across a mossy
valley, and then ascends for some way up the sides of Coul-more,
an enormous denuded mountain-mass of gently inclined Cambrian
sandstone. The white quartz-rock is surmounted by brownish
beds containing fucoid impressions, these again by a band of white
quartz-rock, above which comes a thick white limestone reaching
to the summit of the cliff, where it begins to slope below quartzose

Fig. 2,—Section at Craig-an-Knochan.
Coul More. Road.

Craig-an-Knochan.

&. Cambrian sandstone and conglomerate. ce, Quartz-rock.
el. Quartz-rock. c+, Limestone.
c*. Fucoid-bed. c*. Limestone. d. Gmeissose schist.

micaceous beds, the whole dipping E. or E.S.E. at 10° to 15°. The
details, of course, vary considerably even in the course of a few
yards ; but the general order remains the same, the limestone being
regularly intercalated between a series of white quartz-rocks below,
and a set of quartzose schists (= the Upper Gneiss of previous
papers) above.

This order continues to be observable until the road deflects a
little to the south-east, crossing the limestone, which then plunges
below a series of lonely mountain-tarns, and is not again seen until

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 181

we reach Drumdrynie, about a mile and a half to the south. The
schistose series which covers the limestone, however, is well ex-
hibited along the roadside. It consists of quartzose, micaceous,
fissile, and flaggy strata, to different parts of which the terms
quartz-rock, grit, or mica-schist might be correctly applied. The
general dip isa gentle one to the E. or E.S.E.; and as the road quits
the lochs and winds along the west side of a broad valley, the
strata can be seen to the east, rising terrace over terrace, with the
steep fronts facing the west, and the sloping declivities dipping
eastward, like their component strata.

Drumdrynie——At Drumdrynie Cottage, which lies on the west
side of the road between Inchnadamff and Ullapool, the limestone
again appears. Here, too, it is clearly interpolated between a lower
quartz-rock and an upper quartzo-micaceous series. It is seen on
the gentle ridge behind the cottage; thence it descends, crosses the
stream and the road, and keeps along the roadside as a terrace or
escarpment similar to that of Craig-an-Knochan, but greatly lower.
The succession can be studied with advantage in the stream, and
also along the roadside for fully two miles, where the following
section 1s observable :—

Fig. 3.—Section South of Drumdryme Cottage.

6. Cambrian sandstone and conglomerate. c?. Limestone.
cl. Quartz-rock. d. Gneissose schists.

The strata which repose upon the limestone, when traced across
the hill to the farm-house of Langwell, are seen to be frequently
twisted into crumpled lamine, often highly micaceous. They gra-
duate upward into dark-grey or greenish flaggy beds, which at one
time might be called gneiss, at another mica-slate, at a third clay-
slate; but by far the most abundant material in their composition
is quartz. They are well exposed at the head of Strath-Kennort, a
short way above Langwell, where the river bursts through a narrow
gorge in some picturesque cascades. The strata here are dark and
schistose, with a mass of porphyritic felstone, running parallel to
their strike.

Strath-Kennort.—Strath-Kennort is a valley which extends in
an east-and-west direction from the maritime loch of the same
name to the cascades just mentioned. The limestone, after ap-
proaching within a short distance from the north side of the strath,
is lost under the herbage, though a quantity of fragments and an
old kiln may perhaps indicate its site on that side. On the oppo-

VOL. XVIT.—PART I. o

182 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

site side, however, it is readily apparent by the bright verdure of
the knoll in which it protrudes into the valley.

A small streamlet has laid open the junction of the limestone
(which is here of much greater thickness than where last seen) with
the superjacent beds. The main mass of limestone is greyish or
bluish-white and grey, weathering grey or yellow; but the upper
part is white. It is surmounted here by a bed eight to ten feet
thick of white quartz-rock, which dips below a series of schistose beds
that incline to E. 30° S. at 20°. The band of quartz-rock thickens
greatly towards the N.W., and is marked by veinings of serpentine.
The schistose series is of various shades of green, grey, or white,
micaceous and quartzose, the laminse being much contorted.

The strike of the strata carries them obliquely up the southern
side of the strath ; and we can mark that in their progress the lime-
stone rapidly thins off, while its overlying band of quartz-rock
thickens in a corresponding way. About a quarter of a mile east
of the cascades formed by the descent of the waters from a chain
of small lakes into the strath, a fault has thrown the limestone
150 or 200 feet down the face of the cliff. At the top of the
escarpment, resting on the great lower white quartz-rock, the lime-
stone 1s again seen, but rapidly diminishing in bulk, until, in a few
yellow knobs half-buried in the long brown bent, we lose trace of it
altogether. After a short distance we meet with another band of
limestone along with a series of shales and sandstones. ‘The section
here displayed is partly obscured by a morass, and partly by a fault,
which, however, since it traverses the strike of the beds, probably
does not materially affect the order given in the annexed figure.

Fig. 4.—Section of South side of Strath-Kennort.

ce. Quartz-rock and a band of limestone.
d. Gneissose schists including a bed of limestone.

From the frequent thick covering of peat and heath, it was dif-
ficult to determine the course of the limestones. The beds between
the seams appeared to grow more calcareous, until the whole be-

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 183

came one thick limestone resting on quartz-rock, and dipping below
gneissose flaggy beds. This limestone follows a curved, sinuous
line across the hilly ground to Loch Auchall, now seeming to dis-
appear beneath the vegetation, and then swelling out again into
irregular lenticular mounds and ridges. The curving of the line
of strike conforming in great measure to the contour of the ground,
shows clearly enough that there is no great line of fault here. The
Strata dip to the south-east, and unequivocally pass under a superior
group of thin-bedded micaceous and quartzose schists.

Before quitting Strath-Kennort, it may be well to mention that
this deep valley affords a good illustration of the varieties of form
and colour imparted to a landscape by changes in the character
of its composing rocks. Standing at the lower opening of the strath,
allis sombre and brown. The dull-red Cambrian sandstones, hoary
with lichens, project their rounded edges out of a shaggy mantle
of dun heather and stunted bent. Further up the glen, however,
where the quartz-rock descends upon the slopes, masses of snowy
crag stand out from the dull herbage. Beyond this a bright-green
knoll, protruding from the brown hillside into the browner valley,
reveals the presence of the limestone, while, far away af the head of
the strath, dark crags and grey scars, rising terrace over terrace,
with still the same dull heath between and above them, show where
the upper gneissose beds have begun to set in.

Loch Auchall.—The sections in the deep gorge of the Auchall,
from the lake to the sea near Ullapool, afford a clear exposition of
the order of succession. They have been well described by Pro-
fessor Nicol*; and we cannot resist quoting a passage from his
memoir. ‘On the steep slope,” he says, “first the limestone crops
out, then the serpentine, and above all the gneiss, forming the
summit of the hill, where it dips at 10°-15°, S. 30° E., though
with slight undulations. The rocks may be traced round the south
side of the hill, placing their relations to each other beyond all
doubt. A vertical section through the summit would pass in suc-
cession through the gneiss, serpentine, limestone, quartzite, and
probably the red sandstone.”

The limestone in this section has attained a great thickness. We
estimated it at somewhere about 500 or 600 feet. The “serpen-
tine”’ of Professor Nicol deserves some notice. In his section of
Loch Broom he has represented this rock as a bed intercalated be-
tween the limestone and his “upper gneiss.” And this is un-
doubtedly its true position, although he has subsequently endea-
voured to explain away what he at first regarded as “beyond all
doubt,” by supposing that the “ serpentine” has come up in a great
line of fissure, and that the “ upper gneiss” is not upper gneiss at
all, but the old Laurentian rock brought up by a gigantic fault.

The rock, as seen at Loch Auchall, we should call a porphyry, or
porphyritic felstone with serpentine. It is disposed in rude beds,
under which the limestone dips, and which are ranged in parallel
ridges dipping in the same direction with the limestone. Near the

* Quart. Journ. Geol. Soc. vol. xiii. p. 21.

92

184 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

latter rock it is full of green serpentine, some parts of the mass
consisting almost wholly of that mineral, which becomes less and
less abundant away from the limestone. The chief component mi-
nerals of the greater part of the porphyry are pink felspar and
semitransparent quartz, the latter occurring sometimes in circular
patches. Lastly, at least at one point, the quartz and felspar gra-
nules are distinctly rounded, and the rock contains numerous rounded
pebbles of quartz and jasper, some of which are as large and round -
as walnuts. This same rock occurs also on the shores of Loch
Broom; and the section there laid open will be immediately de-
scribed.

The Upper Gneissose series does not immediately cover the lime-
stone, owing to the occurrence of this felspathic rock; while the
junction-line is still further obscured by a thick covering of peaty
matter. But from the head of the gorge the shelving beds of that
series can be seen along the margin of Loch Auchall, having their
prevalent easterly dip.

Descending the gorge of the Auchall River by the post-road, we
cross the admirable section of the limestone, quartz-rock, and Cam-
brian sandstones described by Prof. Nicol. That geologist also de-
tails the section along Loch Broom; but there are some features in
the coast-line which it seems ncessary to describe here.

Fig. 5.—Section along the North side of Loch Broom.

a. Gneiss. d. Gneissose schists.

4, Cambrian sandstone and conglomerate.

. Quartz-rock. * Serpentinous and felspathic rock con-
c?, Tamestone. taining pebbles of jasper.

Loch Broom.—The town of Ullapool stands nearly on the line of
demarcation between the quartz-rock and the subjacent Cambrian
sandstones. Following the clear natural section along the high
road from Ullapool to the south, we find the quartz-rock in well-
marked beds dipping E. 4° to 10°S8., at 10° to 15°. Towards its
upper part the rock assumes a pink tint in alternate bands of
lighter and darker shades. Annelide-burrows are numerous; and
it is worthy of remark that the tubes are white in the reddish rock,
recalling the aspect of those in many parts of the Carboniferous
rocks, where, from an under surface of shale, dark worm-pipes
ascend into white sandstone. Alternations of argillaceous shale
occur among the quartz-beds ; and at the bridge of Ault Corry we
meet with the limestone. Here, however, it is only about 10 or
12 feet thick, and dips E. 30° S., at 15° to 20°. It is covered by a
bed of what Professor Nicol calls ‘‘ serpentine or felspar-porphyry,”
which, in his section of Loch Broom*, is correctly represented as

* Quart. Journ. Geol. Soc. vol. xiii. p. 22.

1861.] - MURCHISON AND GEIKIE—HIGHLANDS. 185

interstratified between the limestone and a higher micaceous series.
He has since endeavoured to invalidate his first impressions of the
locality, in order to support a theory subsequently embraced by him,
that what he called “upper gneiss” is really the lower Lau-
rentian rock brought up by a great dislocation. To favour this
explanation, he now lays stress upon the eruptive character of this
porphyry, and seeks to show that it has come up in a line of frac-
. ture, carrying up with it the older gneiss. But for this hypothesis,
there is assuredly no foundation in the sections so well exposed
along the shores of Loch Broom. Prof. Nicol’s first reading of the
geological sequence, from which he has since so widely departed, is
the correct one, and so palpable, indeed, that it could not easily be
missed. There are some features of this so-called “ felspar-por-
phyry,’’ however, which deserve special attention, since they bear
on the elucidation of the nature and process of the metamorphism
of the Scottish Highlands, and were carefully examined by one of us
along the sea-margin, the post-road, and the intervening ground.
Where it overlies the limestone, it is a greenish, quartzose, ser-
pentinous rock. Tracing it down to the shore and along the line
of low cliffs, we find the serpentine diminish in quantity, its place
being taken by pink felspar with a plentiful admixture of quartz-
granules. In this part of the rock, small rounded pebbles of red
jasper were observed; and a close scrutiny soon showed that such
pebbles, along with others of white and pink quartz, were abundant,
forming in some places about half of the rock. The weathered
surfaces, owing to the wasting away of the felspar, exhibited a
closely aggregated mass of small rounded granules of pink and
white quartz, which, in not a few instances, were arranged rudely
im rows like lines of stratification. Along the shore-line this rock
was found to become finer in grain, until it passed slowly into a
red sandstone, hardly distinguishable from that of the Cambrian
series, save in its paler colour and more metamorphosed aspect.
This sandstone is followed by a white quartz-rock very crystal-
line, and with no perceptible trace of bedding, though clearly itself
a bed between sheets of darker material. Above the quartz-rock
come greenish felspathic and serpentinous rocks with occasional
quartzose patches, the whole very irregular. These are succeeded
by a white and greenish serpentinous quartz-rock; and beyond
this, the rocks, still serpentinous, shade off into quartzose flaggy
beds with a general south-easterly dip. These range south-eastward
for several miles with the same general inclination, and are in every
respect identical with the quartzose and schistose series already de-
scribed as overlying the limestone from Assynt to Loch Auchall.
This intercalated band of so-called “ felspar-porphyry ” certainly
does not interfere with the regularity of the order of succession.
We do not regard it as igneous at all, further than the gneiss is
igneous. On the contrary, the greater extent of alteration towards
the limestone, the larger amount of serpentine in the proximity of
that rock, the abundant rounded granules and pebbles of quartz
and jasper, the passing of the pebbly zone into sandstone, and of the

186 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Feb. 6,

quartz-rocks into a quartzose flaggy series, seem to us facts which go
far to prove that this “serpentine or felspar-porphyry” is in reality
a highly metamorphosed band of felspathic grit,—the superior degree
of metamorphism being due to the existence of the limestone, and
possibly also to the large amount of felspar in the original rock.

It may be noticed in passing, that along the sides of Loch Broom
the exposed surfaces of rock are usually well rounded, smoothed,
and seratched, the strie running parallel to the direction of the
fiord, i.e. N.W. and 8.E.

From Ullapool the road skirts the shore to the head of the loch,
and abounds in natural as well as quarried sections of the strata.
The quartzose flaggy schists which overlie the metamorphosed band
and the limestone have a steady dip towards the south-east, of about
15° or 20°; sometimes, however, as about four miles south from
Ullapool, they rise to 50° or 60°, but immediately subside again to
their wonted gentle angle. At Fascrianach, about eleven miles from
Ullapool (the first stage on the road to Dingwall), there is an
admirable section both along the wayside and in a deep narrow
gorge on the west side of the road. The strata here are micaceous
quartzose flagstones, many of which seem hardly at all altered ;
indeed, we instinctively broke open the fissile plates, half hoping to
find between them some fucoid or other impressions. The dip is on
the whole south-easterly, at angles of not more than 8° or 5°; but
the beds are here in slight undulations.

At the eleventh milestone the beds are in places irregularly lami-
nated, and split with a tough, uneven, gneissose fracture. They
are penetrated by irregular veins of white quartz, which run slightly
oblique to the planes of bedding, though in a general sense parallel
to them. But even these irregularly foliated bands are both under-
lain and covered by the usual fissile finely-laminated flagstones,
where the layers of stratification are as parallel and unbroken as in
any freestone-quarry among the Carboniferous rocks of the south.

At the branch-road to Dundonald the flaggy beds become darker
and more gneissose, and begin to assume a contorted aspect. The
dip, too, increases, and eventually becomes vertical. We crossed the
great Dirry More to Contin; but over the greater part of this wild
region the rocks are wholly obscured. It appeared to us, however,
that the gneissose beds at the Dundonald road, after bemg crumpled
and contorted in a synclinal axis, probably rise again with a north-
westerly dip. It seems almost certam, at least, that between that
locality and Ben Wyvis there must be many archings, like that on
Loeh Fannich before deseribed*, so. that the same group of rocks is
repeated again and again ; but even then the actual thickness of this
upper quartzose and gneissose series must be admitted to be very great.

Returning to Ullapool, we shall now describe the course of the
lower quartz-rock, limestone, and upper quartzose series towards
the south.

From Loch Broom to Loch Maree.—The region between Loch
Broom and the head of Loch Maree is one of the wildest in the

* Quart. Journ. Geol. Soe. vol. xv. p. 387,

1861. ] MURCHISON AND GHIKIE—HIGHLANDS. 187

North-west of Scotland. There is no road, and for many miles not
even sc much as a mountain-track. Wastes of brown moor and
shaking bog ; glens once inhabited but now desolate ; lonely tarns, the
haunt of the wild duck and the curlew ; and mountain-ranges that
stretch away to the Western Ocean on the one side and the North
Sea on the other, and sweep upward among the everlasting mists—
such are the features of a region that seems never to have been
trodden by foot of geologist. It abounds, nevertheless, with striking
and instructive natural sections. In no part of the North-west
Highlands can the order of superposition be more distinctly seen
than in this wild mountain-tract between Loch Broom and Loch
Maree.

Crossing Loch Broom at Ullapool, the same rocks are found in the
same order, save that the limestone seems not to exist; nor does it
come in again for a long way to the southward. Such disappearances
of the caleareous parts of the series are of frequent occurrence
throughout the whole of the Scottish Highlands, as in the Silurian
formations of England and Wales. The quartz-rock and Cambrian
sandstones sweep over the hilly ground of Ben-nam-Ban, and descend
into the valley at the head of Little Loch Broom, near the Mansion
of Dundonald. From this point they were traced by one of us south-
ward, up the gorge of Corry Hourachan. Here there is a clear section,
which is represented in the accompanying woodcut (fig. 6).

Fig. 6.—Section at Corry Hourachan, South-west side of
Litile Loch Broom.

6. Cambrian sandstone and conglomerate.
c. Quartz-rock. d. Gneissose schists.

The stream has cut a deep channel, partly in the line of junction
of the quartz-rock and schistose series, and partly transverse to it,
the completest possible sections being thus exhibited. At its lower
part the stream runs on quartz-rock; but higher up it is crossed by
this rock, which then forms the western side of the ravine, the upper
schists being peeled off and left as a cliff on the east side. A short
way above this the schists too cross, and sweep up the western side
of the valley. The quartz-rock asceuds for a short way along the

188 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 6,

flanks of the mountain-mass of Kealloch—an enormous denuded
range of gently inclined Cambrian sandstones.

From the head of the Corry Hourachan to the bealloch at the 8.E.
end of Strath-na-Shallag, there is a broken track that winds among
a succession of knolls and crags, rising out of a bare moor, These
show well the character of the passage-beds of the quartz-rock into
the upper quartzose series. No igneous rock was observed in the
whole district; and the metamorphic band of Loch Broom seems to
have died away.

At the head of Strath-na-Shallag, a streamlet descending from
the east has laid open a good section of quartzose grit, argillaceous
shale, and gneissose bands, some of the strata showing annelide-bur-
rows. It seemed a hopeful locality in which to look for fossils; but
our time did not admit of a careful examination of the rocks. Lime-
stone was formerly worked here ; but the bed escaped our search.

Ascending the valley of Loch Ned, a section occurs similar to that
of Corry Hourachan. The east side of the glen is capped by the
upper gneissose beds; below these comes the quartz-rock, which in
turn rests on the Cambrian sandstones that occupy the bottom of
the valley, and rise up into the group of mountains lying between
Loch-na-Shallag and Loch Maree. As we ascend the valley, the
quartz-rock descends into the bed of the stream, and then begins to
ascend on the western side, stealing up the hillside, the imclination
of which nearly corresponds to the angle of dip of the beds. The
eneissose beds have been swept out of the bottom of the valley, but
they oceur as outliers on the western side. Of this there is one
striking example a little above Loch Ned. The eastern slopes of Scour
Van slope down to that lonely tarn, and their lower parts are coated
with quartz-rock. A stream here descends in a series of cascades,
which, from the snowy tint of the quartz-rock and the sombre hue
of the Cambrian sandstones that form the higher grounds, are ren-
dered eminently picturesque. The watercourse for some way runs
on inclined planes of quartz-rock, above which, in distinct super-
position, are two dark peaks, outliers of a greenish serpentinous
and actinolitic gneissose rock, with veins of red felspar (fig. 7). The

Fig. 7.—Section at Loch Ned.

Ce _
6. Cambrian sandstone and conglomerate.
e. Quartz-rock. d. Gneissose schists.

1861. ] _ MURCHISON AND GEIKIE—HIGHLANDS. 189

scenery of the Loch Ned Valley affords another excellent illustration
of how closely the physical aspect of a country is linked with its
geological structure.

Beyond the head of Loch Ned the glen bifurcates,—the eastern part,
or that to the left, leading to Loch Vrin, and thence to the Ullapool
road at Fascrianach, while the western branch ascends by the Beal-
loch-na-Cros to Loch-na-Fad. The latter glen has been deeply cut
by a mountain-torrent ; and its sides are likewise scarred and grooved
by watercourses, which, though usually dry, or nearly so, are rapidly
filled by the rains which sweep down the declivities, leaving the
bottom of the pass strewn with débris. Red felspar is here espe-
cially abundant, mingled with a dark chloritic gneissose rock.

Ascending to the summit of the Bealloch-na-Cros, over heaps of
rubbish in which felspar fragments are especially numerous, we
have a wide view of the surrounding mountainous ranges. The
rocks on either side have a decided easterly dip on the sides of the
glen and along the slopes of the adjacent hills, especially those which
encircle the gloomy Corry Vichkerracher (Farquhar’s Corry). The
sheet of water called Loch-na-Fad lies before us. Beyond it, to the
west, rise the enormous masses of Cambrian sandstone and Lauren-
tian gneiss that form Sleugach and the neighbouring mountains
which shoot up from the depths of Loch Maree.

A little on the west side of the upper part of the bealloch, a ravine
exposes the white quartz-rock, dipping a little north of east, at
10-15°. From this point to Loch-na-Fad, the descent lies over
mounds of débris of white quartz-rock and red felspar. Both these
rocks protrude in detached hummocks and knolls. Near the lake,
the felspathic rock becomes serpentinous, and we then, at the south
end of the lake, come upon a limestone of considerable thickness,
dipping to the north-east. We were informed that limestone was
worked at the north end of the loch, at a place called Glen Tulloch,
but not in so thick a bed as that of Loch-na-Fad. The latter we
regard as a continuation of that seen in Glen Cruchalie, which will
presently be described.

That this limestone occupies, on the whole, the same horizon as
that of Ullapool, Drumdrynie, and Assynt, can hardly be doubted.
The amount of drift by which it is surrounded, however, does not
admit of a close examination of its junctions with the adjacent rocks ;
while the time at our disposal proved much too short for such a
serutiny as this portion of the line of outcrop deserved. It is quite
possible that there may be some faulting here, and even to a con-
siderable extent, though the general order of succession remains
sufficiently clear. The metamorphism which is often most intense
in the vicinity of a limestone is conspicuous here. The serpentine
increases aS we approach the calcareous beds; and, did the drift-
covered surface permit, we might in all likelihood find the one rock
passing insensibly into the other.

Below the limestone lies the usual white quartz-rock, creeping
up the acclivity on the west side of the loch, with a gentle north-
easterly dip. The lake empties itself by the River Hassac, which,

190 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

flowing down a deep, precipitous gorge, enters the head of Loch
Maree. Where the stream quits Loch-na-Fad, the Cambrian sand-
stone sets in, extending up the loch and down the river, and rising
up into the great mountain-masses already referred to. The descent
of the ravine of the Hassac, by a tortuous and usually imperceptible
track, brings before the geologist a noble natural section. On the
south, or left side, the Cambrian strata rise for some way up the
cliff, capped by the white and grey beds of quartz-rock. On the
other side the latter strata are absent, and the Cambrians form the
craggy scarps of the ravine, till they are succeeded further down by
the subjacent Laurentian gneiss.

Loch Maree-—Loch Maree, one of the wildest of Scottish lakes,
presents a series of sections of singular clearness. With Kinloch
Ewe as his head-quarters, the geologist has a wide sweep of in-
teresting ground around him; and we know of no locality where he
may better acquaint himself with the order of superposition of the
ancient crystalline rocks of the Highlands, or with the dislocations
and metamorphism which they have undergone (fig. 8).

The occurrence of the Laurentian gneiss on the banks of this lake
has been already described in this memoir, as well as the superjacent
Cambrian sandstones, and the inferiority of these to the white quartz-
rock. From the mouth of the Hassae river, up the valley, to the
opening of Glen Cruchalie, the quartz-rock forms the north-eastern
side of the valley ;, for the Cambrian strata rapidly dip below the
surface. <A felspathic rock, however, occupies the lower part of the
cliff, and even rises to a considerable height above the valley. The
same, or a similar mass, occupies, as we shall immediately see, a
large part of Glen Cruchalie.

The quartz-rock dips in a south-easterly direction, at various
angles, up to 35° or 40°. It is worthy of remark, that it extends
further south-east on the northern side of Loch Maree than on the
southern. On the former it continues to the line of Glen Cruchalie,
where it is overlain by the limestone; on the latter it ends at or
near the Inn of Kinloch Ewe, where, in the bed of the stream, are
flagey gneissose beds, indicating the upper series. The strata on
the one side of the valley, if prolonged across, would abut against
the edges of a different set of strata. Either, therefore, there must
be a very sharp and sudden change in the strike of the rocks between
Glen Cruchalie and Kinloch Ewe, or a fault must traverse the valley
along the line of Loch Maree. The latter explanation is probably
the true one. This fault, however, it is needless to remark, does
not in the least degree obscure the order of succession.

The upper beds of the quartz-rock are well exposed in Glen
Cruchalie. They dip south-easterly, at 35°, and show large surfaces
covered with annelide-burrows. They are immediately succeeded by
beds of bluish-grey and red mottled limestone, with shaly bands,
having the same general inclination.

In Glen Cruchalie the most marked rock is one similar to that
which was described as overlying the limestone at Loch-na-Fad,
and underlying the quartz-rock at the mouth of the Hassac and

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192 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

along the higher part of the valley of Loch Maree. It is difficult to
give this rock any one specific name; for, like that in Sutherland,
which we formerly described*, it varies greatly in mineral composi-
tion, even within a few yards. Near the limestone it is a serpentine ;
the green mineral then thins away, and quartz and felspar take its
place, while to these is occasionally added hornblende. The propor-
tions of the ingredients also vary to a large extent.

This rock, by whatever name we designate it, occupies a large
part of Glen Cruchalie. Sometimes it lies only along the bottom of
the glen; then it rises high on the one side, and soon ascends among
the slopes on the other. In some places it occupies indifferently the
place of the limestone, in other parts that of the quartz-rock or the
upper flaggy series, or it invades the three zones at once. But, though
it forms an important feature in the geology of the district, and oc-
cupies a considerable area, it does not interfere with the ascending
order, which is here, as everywhere to the north, quartz-rock, ime-
stone, and upper flaggy or schistose beds.

The latter series of strata can be examined with advantage up the
ravine, along which the road winds from Kinloch Ewe to Auchena-
sheen. It consists of quartzose and micaceous flagstones and schists,
the south-easterly dip of which is well seen along the higher slopes
of the glen, the angle yarying from 25° to 50° ‘These rocks clearly
overlie the limestone, and are as dissimilar lithologically to the Lau-
rentian gneiss (with which Professor Nicol would identify them) as
two groups of strata can well be.

Loch Maree to Loch Torridon.—Few mountains in Scotland present
a more striking aspect than those which close in around the head of
Loch Maree, and stretch westwards to the Atlantic. Giant, sombre-
hued masses of Cambrian sandstone, in nearly horizontal beds, rise,
band over band, to a height of fully 3000 feet. Their summits are
not unfrequently capped with white quartz-rock ; and under certain
phases of the sky, when a gleam of sunshine falls on these hill-tops,
they seem in the distance as if tipped with snow. The illusion is
sometimes heightened by the faults, which let down the quartz-rock
in wedges among the dark-hued Cambrian beds; for then the white
crags, descending some corry with a long stream of grey rubbish
below them, look like a stunted glacier, or an incipient avalanche.

The general aspect of these hills is shown in the preceding dia-
grammatic section from the sea at Loch Torridon, across Loch Maree,
to Loch-na-Fad (fig. 9). The same geological characters mark the
high ranges from Leagach and Ben Eay to the Dingwall road at
Craig Inn. Some of the features of this tract it is necessary to
advert to more in detail. The rocks are faulted in a very extra-
ordinary manner ; and these dislocations have been supposed to lend
some countenance to the hypothesis that the upper gneissose series,
which rests on the limestone, is the Laurentian gneiss, brought up
from the bowels of the earth by a convulsion of unknown magnitude.
It would indeed be strange if, in a country so metamorphosed and
mineralized, presenting so many crumplings and contortions of the

* Quart. Journ. Geol. Soc. vol. xvi. p. 238.

1861.] MURCHISON AND GEIKIE—HIGHLANDS, 193

strata, and abounding in so many deep gorges and ravines, there
were yet no lines of extensive faulting. Such lines must almost
necessarily exist. But what are the conditions needful for their
discovery ? Must we not have at least certain persistent strata of
well-defined lithological characters, and trace them in their windings
among the mountains? Such strata, however, are not well repre-
sented among the Silurian rocks of these regions. The limestones,
as we have seen, are subject, as in Wales and Siluria, to sudden
and capricious changes, amounting even to entire disappearance.
The upper gneissose series has no distinguishing band, and, where
the limestone is wanting, passes down imperceptibly into the quartz-
rock. The quartz-rock, too, has a more or less uniform aspect
throughout ; so that faults, repeating one part of it against another,
might easily escape observation. If, however, we could find it on
some exposed hillside, faulted along with its subjacent Cambrian
sandstones, there would then be every probability of detecting the
fractures ; for the quartz-rock being white, and the Cambrian dark
reddish-brown, any alternation of these two formations would be
observable even at a distance. This desideratum is admirably sup-
plied among the craggy mountains of Beann Taobhliath, which, from
within four or five miles of Loch Maree, extend southwards almost to
Loch Doule, on the road between Dingwall and Skye. The hillsides
along the deep glens in that region afford the clearest and most
startling proofs of dislocation; and yet, but for the contrasting co-
lours of the two series of rocks, these fractures would probably never
have been detected, unless, with a good map in his hand, a geologist
had set out purposely to seek for them. Hence it is in the highest
degree probable, that among the gneissose rocks there may exist many
large faults, which have not been even suspected.

Having made this admission, however, it by no means follows that
over the region we have examined any kind of fault may occur, and
along any part of the line. In the sections already described in
this paper there is certainly no fault, but a clear order of superpo-
sition from the lewer quartz-rock into the upper quartzose or gneiss-
ose series. But between the points which we have selected for
description in detail, it is far from improbable that faults may inter-
vene, limited in their extent and in their amount of throw. They
can only be local; and their character is probably sufficiently shown
in the region, one or two sections in which we shall now describe.

Beann Taobhhiath, or “the Grey Heads.”’—About 5 or 6 miles south-
west from Kinloch Ewe, on the road to Loch Torridon, lies the water-
shed between that arm of the sea and the freshwater Loch Maree.
On the north side of the valley the mountains of Leagach and Ben
Kay, already referred to (fig. 9), show their capping of white quartz-
rock on the sombre-hued Cambrian sandstones which form their
mass. It was the southern side of the valley, however, that chiefly
attracted our attention. There the quartz-rock on the mountains,
when seen from the road, appeared interbanded with some dark rock,
as if sheets of greenstone had been thrust between its strata. This
seemed the more inexplicable as we had seen no such rock in any

194 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

other part of the district, and none certainly which showed such a
regularly stratified arrangement. One of us, accordingly, ascenaed
the craggy sides of Scuir Dhu, and thence obliquely southwards to
the top of the highest of the Beann Taobhliath hills, or “Grey
Heads.” The following section represents, better than any detailed
description, the structure of Scuir Dhu.

Fig. 10.—Section of Seuwir Dhu.

b. Cambrian sandstone and conglomerate. c. Quartz-rock.

The Cambrian at the base of the hill dips E. 10° to 20° 8., at 30°
to 40°. It is covered by white quartzite having the same dip and
angle, and showing still the oblique lamination or “ false-bedding ”
of the original sand. Did no other section exist, we should say that
the Silurian rocks here followed the Cambrian in conformable se-
quence. The Cambrian beds slope up the valley along the lower part
of the acclivity, while the quartz-rock rises above them to form the
greater part of the north-eastern side of the glen. The latter rock is
occasionally deeply channeled by mountain-torrents. One ravine
in particular occurred in the course of the ascent, about 80 or 100
feet, and, in places, so narrow that it seemed as though one could
almost have stepped across it. Cambrian blocks strew the hillside,
and are often perched on the edges of cliffs and on the summits of
detached crags. None of them are of great size, the largest observed
being eight feet long, six broad, and three high. Gneiss-boulders
also occur, but are small in size as well as few in number. The
quantity of Cambrian blocks increases as we ascend, until, not far
below the summit, we come upon a mass of Cambrian sandstone in
place, dipping E. 4° 8., at 27°. Between the quartz-rock and this
Cambrian ledge there is undoubtedly a fault, the former rock having
its beds curved and thrown back against the latter: this is shown
in the subjoined section (fig. 11), which is an enlarged view of that
part of fig. 10, marked *. The Cambrian beds are then covered
over by flat undulating beds of quartz-rock, which lie at the base of
a cliff of similar Cambrian sandstones. At the top of this cliff a small
ledge of quartz-rock exists (as shown in fig. 10), let in by a fault

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 195

below another Cambrian crag, above which comes a snowy cliff of
quartz-rock, forming the summit of the mountain.
The Cambrian rocks support hardly any vegetation, the quartz-

Fig. 11.—Enlarged Section of the Point marked * in Fig. 10.

6. Cambrian sandstone and conglomerate. ce. Quartz-rock.

rock still less. There is, therefore, no obscuration of the lines of
junction, save such as arises from the débris of the crags, worn down
as these are by the rains and frosts of winter, that tell especially
upon the quartz, splitting up its beds and covering its surface with
piles of loose, rough, angular blocks, on which it is often perilous
to tread. There is no difficulty in determining which are lines of
fracture and which lines of regular superposition : the section, indeed,
is nearly as distinct as it can be drawn on paper. The uppermost
ledge of red sandstone dips EK. 4° to 10° S., at 30° to 36°; the
quartz-rock which covers it dips E. 4° to 10° S., at 35° to 42°.
These figures are given as the mean of several observations made at
intervals along the exposed ledges. They show that, in a general
sense, the two series of deposits are conformable ; and this conformity,
could we obtain unweathered surfaces for careful measurements, might
be shown to be complete. It is sufficiently evident, however, that
this undisturbed sequence is accidental, and that the Cambrian beds
had undergone erosion previous to the deposition of the overlying
deposits. - In no instance is there anything like a passage of the one
series into the other ; on the contrary, everywhere along the junction
the line of demarcation is sharp and defined. Such sections as that
given in the annexed figure (fig. 12), are not uncommon where a

Fig. 12.—Section showing the Junction of the Quartz-rock and the
Cambrian Sandstone on Scurr Dhu.

6. Cambrian sandstone and conglomerate. e. Quartz-rock.

bed of red sandstone has been at one point eroded, and is there un-
conformably overlapped by the quartz-rock.

196 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

From the summit of the hill the
quartz-rock plunges down the north-
eastern side towards the valley of Loch
Clare; but the Cambrian again comes
in, owing to the intervention of other
faults. Crossing along the ridge to
the next hill to the south, we meet
with other examples of the apparent
interbedding of quartz-rock and red
sandstone. There is a gorge or bealloch
(of which we could not ascertain the
name, and it is nameless on the maps)
on this ridge, having a stream on the
east side, which descends into Loch
Coulan, and another on the west, that
falls into the valley of the Torridon
Water. Following the line of the glen
on the south-east side, we are pre-
sented with one of the most striking
natural sections anywhere to be seen
in the North-western Highlands. The
alternations of red sandstone and
white quartz-rock are repeated again ;
but here, in place of merely an out-
crop-line along the strike, we have a
magnificent transverse section several
hundred feet deep, along the southern
side of a wild glen. The contrasting
tints of the two rocks give the decli-
vity all the appearance of a vast dia-
gram; and no diagram could repre-
sent the dislocations in a more im-
pressive manner. The subjoinedfigure
(fig. 13) was copied while we walked
down the glen, andrepresents, asnearly
as may be, the actual relations of the
rocks. We may add, that the same
dislocations cross to the north side;
but the greater amount of débris on
that side makes them less easily trace-
able. They undoubtedly run both
north and south of the glen; and
these mountains have thus the sin-
gular aspect of alternating cliffs of
snowy whiteness and sombre brown.
We could mark the arrangement on
the hills a short way north of the
Dingwall road at Loch Doule, a di-
stance of fully ten miles from Ben
Eay, where similar dislocations were

Length 2 miles.

Fig. 13.—Sectional View of the Dun Tolleah Hills.

[Feb.

Fault.

Fault.
Limestone.

Fault. Fault.
cl, Quartz-rock.

’. Cambrian sandstone and conglomerate.

d. Gmeissose schist.

c?,

od

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 197

also observed. The map of this region would therefore represent a
series of irregular strips and patches of Silurian quartz-rock, inserted
among Cambrian sandstones by the agency of longitudinal faults
which seem to split off from or coalesce with each other.

Towards the lower end of the valley the quartz-rock dips E. 10°
S., at 35°, and is followed by a band of limestone conspicuous from
the neighbouring hill-tops, owing to the bright verdure that marks
its course. Above the limestone come beds of quartz-rock and
quartzose flagstone; and these, becoming more and more schistose,
eross Loch Coulan, and are seen in the ravines and watercourses on
the opposite side. They form, of course, the upper quartzose series
so frequently referred to. j

The region lying between the Grey Heads and Loch Doule has
never been explored. We were able to see its general structure from
some of the neighbouring hill-tops; but it must contain much in-
teresting detail to reward the fatigues of an enterprising geologist.

Loch Carron.—After traversing this faulted district, the quartz-
rock approaches Loch Doule, whence it bends towards the south-
west, occupying the high ground on the north-west bank of Loch
Carron. At the head of the latter loch it is overlain by a limestone,
which extends for some way towards Jeantown, until lost beneath the
alluvial accumulations of the valley.

The road from Jeantown to Applecross crosses a high ridge, and
descends to Loch Keeshorn, through a ravine in which there is a well-
exposed section of the strata. First, on leaving Jeantown, we have
schistose beds with a south-easterly dip; these gradually pass down
into a quartzose and flaggy series, which towards the lower end of the
ravine are underlain by the quartzite. The next rock in descending
order is a limestone of great thickness, which occupies the south-.
eastern side of Loch Keeshorn*. It dies rapidly away to north, and
a short way beyond the head of the loch has disappeared altogether.
It is underlain by white quartz-rock, which, coalescing with that
above the limestone, forms one series, below which lie the Cambrian
sandstones swelling up into the great mountains of Applecross and
Loch Duich.

We had not time fully to work out the relations of the Keeshorn
limestone: possibly it may be the same as that of Loch Carron,
Loch Coulan, and Glen Cruchalie—that is, the limestone zone between
the lower quartz-rock and the upper quartzose flaggy series ; or, like
the lower limestone of Ben Kay, already referred to, it may be a local
deposit occurring in the lower quartz-rock. The area which will
decide this point is the high ridge on the northern side of the Loch
Carron Valley, between Lochs Keeshorn and Doule.

The sections along the shores of Loch Carron at Strome Ferry are
singularly clear. They show the quartzose flagstones in well-defined
beds, dipping sharply to the south-east at 45° or more. The same
rocks occupy the intervening tract of land to the Kyles at Balma-
carra, where another admirable line of section can be examined along
the shore.

* See Nicol, Quart. Journ. G. S. vol. xiii. p. 29: Murchison, 2. vol. xv. p. 188.
VOL. XVII.—PART I. P

198 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

Loch-alsh.The promontory opposite Kyleakin has hitherto been
mapped as “ Red Sandstone,” lke the hills of Applecross, that is,
“Cambrian” according to our classification of these rocks. Next to
this red sandstone, there has been inserted on the east side a strip
of quartz-rock, beyond which, at Balmacarra,comes the great“ gneiss”
region of previous geologists*. The red sandstone, however, is not
identical with that of Applecross, or the red sandstone of the west
coast generally ; indeed, so far as we observed, it is rarely red
sandstone at all, but greyish quartz-rock, which assumes a pink or
reddish tint, chiefly on the weathered surfaces. It has an E.S.E.
dip at gentle angles. Opposite Kyleakin, indeed, there is a confusion
of the bedding, owing perhaps to the prolongation of a fault from
Skye, to be immediately noticed; but east from this the stratification
becomes quite regular. The quartzy flagstones, in well-defined beds,
dip steadily up Loch-alsh, at from 15° to 20°; towards Balmacarra
House, interlaminations of shale or schist begin to appear; and these
continue to increase, imparting a fissile character to the strata. As
we trace the strata still eastward, their schistose structure increases,
until, by the diminution of the quartzose bands, and the greater de-
velopment of the argillaceous and micaceous portions, they insensibly
pass upwards into schists and gneissose rocks ; these range eastwards
up Loch-alsh, with here and there a boss of syenite, or felspar-por-
phyry. No clearer evidence could be desired, that the quartz-rock
or quartzose flagstones graduate in perfect lithological sequence into
the upper schists.

In Sutherland, as stated in former memoirs, the quartz-rock above
the Assynt limestone is superposed by another limestone, which,
however, is of no great continuity. We failed to detect it in any of
the transverse sections of the country between Assynt and Loch-
alsh. Along the shores of Loch Duich, however (which is a branch
of Loch-alsh), the schists that overlie the upper quartzose flagstones
contain, in their lewer part, several limestone bands, in the same
way as the Sutherland limestone lies between the upper quartz-rock
and the superjacent gneissose rocks.

Loch Duich.—The Loch Duich limestones are best seen along the
south side of the fiord. There are at least five or six bands having a
general easterly or south-easterly dip. They are separated by talcose,
actinolitic, and micaceous schists, often serpentinous like the lme-
stones themselves: red felspar-porphyry and syenite also occur in
bosses, dykes, and veins. The longest beds of limestone are perhaps
those of Totig Point, opposite the village of Dornie and Eilan-Dou-
nan; there they are sometimes pure white, with green serpentine
streaks, and have been quarried on the shoret. They range across
the hills into Glenelg.

Red felspathie rocks abound chiefly towards the head of Loch
Duich ; they are conspicuous in the hill of Mam Rattachan, and
likewise in many of the gullies and clefts worn on the hillsides by
the rains, as well as on the shore. We found them also among the

* See especially Prof. Nicol’s map, where these errors are to be seen.
t See Quart. Journ. Geol. Soc. vol. xiii. p. 30.

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 199

flaggy beds of the Bealloch of Kintail, which, with a south-easterly
dip, range northwards to the deep gorge of the Glomach, where, in a
scene of singular wildness and grandeur, the stream, in falling over
the cliffs, gives rise to the highest cascade in Scotland.

Skye.—Following the line of outcrop of the Lower Silurian quartz-
rock and limestone, we have arrived at the shores of the Atlantic.
But these rocks are prolonged into the Island of Skye; and before
tracing the structure of the interior of the mainland, we will sketch
in outline that of Sleat—the southern peninsula of Skye.

In a former memoir*, it was shown that the Lias of Strath, in
Skye, rested unconformably upon red (Cambrian) sandstone, and
that the sandstone stretched across the island from sea to sea, with
a north-westerly dip. It was also pointed out, that some powerful
faults existed in the district, whereby the secondary shales and lime-
stones were thrown down in wedge-form among the older strata. We
have now ascertained that the same faulted character extends across
Loch Eishort into Sleat, rendering the geology of that peninsula in-
tricate and difficult. With the limited time at our disposal, and the
want of a map having any approach to accuracy, we did not attempt
to work out the detailed structure of this region.

Sleat appears to have formed originally, previous to the occurrence
of the faults, an anticlinal ridge consisting fundamentally of Cam-
brian sandstone with the quartz-rock, limestone, and upper gneissose
beds folded over it. Traces of this simple structure are sufficiently
abundant; but it has been greatly modified and deranged by the
influence of certain longitudinal dislocations, by which the north-
western side of the arch has fallen in; and considerable confusion
has been introduced into the southern end of the peninsula.

The Cambrian, rising from under the Lias, forms the north side of
Loch Eishort and runs across to the Bay of Lussay. From the head
of Loch Eishort a fault extends to the shore near Kyleakin, the effect
of which is to throw down the quartzose flaggy beds against the
Cambrian sandstones, both of which have a north-westerly dip.
Another fault runs probably from about Kyleakin, along the north-
west flank of Ben Cailleaich, towards the Point of Sleat, with the
same effect as the other; so that the arch becomes still further frac-
tured towards the south-west end of the island.

At Ord the red sandstones are also considerably faulted. On the
hills above the House they are surmounted by quartz-rock in thick
beds of snowy whiteness. These dip north-west, at a steep angle,
forming the side of a steep hill, at the bottom of which they are
covered by limestone, evidently on the same horizon with that of
Assynt and Loch Broom.

This limestone appears to be surmounted by quartz-rock ; but this
part of the island is dislocated to no common extent, and would
require much care and time in the unravelling of its details rf.

* Geikie, Quart. Journ. Geol. Soe. vol. xiv. p. 1 e¢ seg.

+ I am now convinced that the white quartz-rock noticed in my former paper
as wedged in at the side of a fault on the shore of Loch EHishort really belongs
to this Lower Silurian series, and is therefore the product of a much older meta-

PQ

200 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

Returning to the shore opposite Balmacarra we find that the
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western side of the anticlinal arch is obscured by the faults ; but their
south-eastern dip is well shown along the bare grey slopes of the
morphism than that of the Lias limestones. It occurred to me also, lastsummer,

while on the hills above Ord, that possibly some parts of the metamorphic lime-
stone of Strath may possibly be also Silurian.—aA. G.

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. _ 201

hills. The same dip continues by Kyle Rhea along the south-eastern
shore of the island, which is traversed by numerous N.W. and 8.E.
dykes of greenstone. The same reddish tint is here observable that
was noticed in the description of the Balmacarra flagstones. The
cause is the same in this case also; the red colour is a mere crust
owing to the oxidation of some of the component minerals ; while the
rock, when broken, is grey or white within.

At Isle Oronsay, as at Balmacarra, we found a gradation from these
flagstones into the upper gneissose or schistose series. These schists
have a south-easterly dip, but are much crumpled in places. Near

6. Cambrian sandstone. d. Gneissose and schistose rocks. jf. Fault.

Knock a good section is obtained from the shore inland, showing the
curving of these strata, and about halfway between Knock and Ord
they are seen to graduate as usual into a lower series of quartzose
flagey beds.

2. Structure of the country between the Atlantic and the line of the
Great Glen—Haying traced the southward prolongation of the
quartz-rocks and limestones in Skye, until they are lost beneath the
waters of the Atlantic, we now give the results of several traverses
of the region to the east of these rocks, in order to show the cha-
racter of the upper gneissose series of deposits and the geological
structure of this part of Scotland. In former memoirs upon the
rocks of Sutherland, reference was made to the great apparent thick-
ness of the flaggy schistose strata which there overlie the upper lime-
stone and form the central and eastern portions of that county. The
thickness was indeed so great as to compel the belief that many
folds must necessarily exist, even although in most of the observable
sections the rocks continued to plunge towards the south-east. But
the data were wanting on which to speculate as to the character and
amount of such folds. This summer, however, we were fortunate
enough to obtain some illustrative sections which showed how de-
ceptive this steady south-easterly dip might really be, and how pro-
bable it was that, even where no change in the direction of inclina-
tion could be traced, the strata might nevertheless be repeated upon
themselves again and again.

Loch Broom to Contin.—One of us continued the section from Loch
Broom across the wild uplands of the Dirry More to the Old Red
Sandstone of the east coast, where it ascends the River Conon to
Contin. The amount of alluvium along the valleys rendered the
greater part of this traverse unsatisfactory; but enough was ob-
served to justify the belief that when this region is properly mapped
it will be found to contain many anticlinal and synclinal folds as

well as local contortions of the strata. The flagey and gneissoseé

202 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Feb. 6
b)

beds from Inisbae to Contin have, on the whole, a south-easterly
dip. On the shores of Loch Garve the gneiss is crumpled into in-
tricate folds; but the prevalent dip is still south-easterly, and con-
tinues so until the Old Red conglomerates supervene at Contin.
Alternations of micaceous gneiss, mica-schist, and grey quartz-rock
form the prevailing rocks of the district. From Contin we recrossed
the country to Loch Carron. The same gneissose schists and quartzose
flagstones were observed along the road, with a general south-easterly
dip, but with several visible folds and many covered parts where a
north-westerly dip may occur, like that of the mountain Aigean on
Loch Fannich, before described*.

Loch Hourn by Loch Quoich to the Caledonian Canal. — We
examined also a line of section from about the middle of Loch Hourn
to Loch Oich in the Great Glen. The rocks which form the mag-
nificent jagged mountains that overshadow Loch Hourn are dark
micaceous flagstones. They have a general south-easterly dip at
high angles and are usually flat-bedded and regular, though some-
times locally crumpled. They occur all up the wild gorge or pass
that rises from the head of the loch to the height of 1000 feet in
the space of a mile. The top of this pass forms part of the main
ridge of the country, and presents the singular phenomenon of a
watershed only a mile distant from the sea on the one side, and
fully fifty miles on the other. All the crags and rocks along the
sides of the pass have been smoothed and striated, by glacial action,
on the faces that look up the glen, while these which point down to
the sea are rough and irregular. ‘There is no drift in the glen nor
at the head of Loch Hourn.

From the top of the pass to the bend of Loch Quoich the same
rocks continue in the same south-easterly inclination. Near Mr.
Ellice’s house at Glen Quoich +, however, a line of synclinal axis
crosses the lake and runs northward to Glen Shiel, where we found it
well marked. On the east, or rather east-south-east of this line (for
its direction is nearly north-north-east), the strata are reversed to
the north-west, and this dip continues along Loch Quoich and for
several miles to the eastward. They then undulate and become ob-
secured partly by granite masses and partly by the deep sandy accu-
mulations of Glengarry, so that their relations towards the Great Glen
were not satisfactorily ascertained. At Invergarry Inn, however,
only about two miles from Loch Oich, the gneissose rocks had a de-
cided north-westerly dip.

The most instructive sections along this line of country were
those in Loch Hourn, and on the road between that deep fiord and
Tomdoun Inn. We would especially instance two rocks or cuttings
on the wayside; one about three miles west from the house of Glen
Quoich, the other at the seventh milestone west from Tomdoun Inn.
The first of these shows in the clearest possible manner how deceptive

* Quart. Journ. Geol. Soe. vol. xy. p. 387.

+ Since our visit to Glen Quoich, our hospitable host, the Rt. Hon. Edward
Ellice, has acquired all the lands of Glengarry, so that his estates now range from
Loch Oich to Loch Hourn, a distance of about 50 miles.

MURCHISON AND GEIKIE—HIGHLANDS. 203

~
[e.8)
(op)
pear
ey

a prevalent dip in this region may be,
even though it should seem to be
perfectly regular. The strata, con-
sisting of gneiss, mica-schist, and mi-
caceous quartz-rock, are exposed for
about 100 yards, and, as shown in the
accompanying diagram (fig.17), are
folded upon each other in such a way
that the same stratum is repeated
seven timesin that space. The actual
thickness of the beds in this section
is perhaps not more than 10 or 15
yards—that is, from a seventh to a
tenth of their apparent thickness. In
walking over the edges of these highly
inclined strata, with possibly here and
there the indication of asouth-easterly
dip, we might very naturally set down
Av =e the beds as one continuous series; and,

Z without a clear transverse section, it
would be difficult to prove that they
were not.

The other section is represented in
fig. 18. It shows another way in
which the vertical thickness of these
upper gneissose rocks may be reduced
from its enormous apparent magni-
tude. Instead of vertical folds, we
are often presented, as in the rocks
depicted in this figure, with contorted
bedding, which even more than the
former tends to modify our estimate
of thickness.

There can be no doubt that these
sections are truly typical of the struc-
ture of the metamorphic regions of
Scotland. Theyshow us how the rocks
are folded on the small scale, while the
synclinal axis of Loch Quoich proves
how these are repeated by great
troughs and arches. The large amount
of repetition thus induced makes it
no longer difficult to conceive that the
eneissose and micaceous flaggy rocks
of the Highlands do not attain so gigantic a thickness as they for-.
merly seemed to do, and that in truth they need not be regarded. as
more than equal to the lower half of the Silurian system in other
regions,

Arisaig to Banavie—A transverse section which we examined
with great care, and which perhaps offers the best natural expo-

Fig. 17.—Seetion showing Contorted Schists and Quartzose Beds (belonging to Series d) near Quoich Lodge.

204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. Feb. 6,

sures of the rocks, is that from the wild headlands of Arisaig to
the entrance to the Great Glenat Banavie. At Arisaig we found the
quartzose flagstones with a W.N.W. dip, traversed by innumerable
greenstone dykes having a north-westerly direction. The same
direction of dip continues along the road a mile and a half to the
east of the village of Arisaig*. The strata are then reversed to the

Fig. 18.—Section of Rocks on the Roadside at the 7th Milestone
west from Tomdoun Inn.

S.E. for about half a mile, after which they undulate in both direc-
tions, as is well shown along the crags near Borrodale, on Loch na
Nuagh. Dykes of greenstone with a N.W. strike still abound. At
the head of Loch na Nuagh the strata of micaceous quartzose schist
have a 8.E. dip at high angles. This inclination continues to near
Loch Aylort, where the beds are vertical, sometimes leaning to the
one side, sometimes to the other. Where the road descends upon
that arm of the sea, the dip is south-easterly ; but it is immediately
reversed to the north-west. From the point whence the road
diverges from the loch, the vertical and contorted strata are seen to
be convoluted in rapid arches; after which, on again reaching the
sea-margin, the dip is south-easterly.

At Kinloch Aylort, highly micaceous quartzose rocks, in well-
marked vertical beds, strike N. 10° E., which exactly resemble those
of Loch Hourn, showing the same alternation of grey quartzose
bands with others strongly micaceous, but without the admixture
of felspar. They are in places true mica-schists, in others quartz-
rocks. The glaciated surfaces are here very apparent,—the vertical
strata being smoothed and deeply grooved across their truncated
edges ; the direction of the groovings runs W. 30°-40° 8.

About a mile and a quarter from Kinloch Aylort the schists are
overlain by a band of quartzose flagstone, well bedded, and in some
beds micaceous and fissile. The dip is exposed in a quarry by the
roadside, being E. 30° 8. at 77°.

From this point onward to the head of Loch Ailt, another series
of micaceous quartzose schists occurs. The inclination is at high
angles, often vertical. The strata are sometimes beautifully con-

* This is the Clanrannald country, now possessed by Mr. Dukinfield Astley.

1861. | MURCHISON AND GEIKIE—HIGHLANDS. 205

~
torted, as at Ault Namuie, where they are curved and convoluted as
at Loch Quoich, though the prevailing dip is still south-easterly.

At the watershed we begin to meet with a reversed or N.W. dip.
The same micaceous strata are again traversed, with here and there
a knob of quartzose granite. About a mile east of the watershed,
contorted rocks are exposed in the bed of a stream which is crossed
by the road.

At the foot of Glen Finnan, near the spot where Prince Charles
first unfurled his flag, the dip changes to N., and then immediately
to N.W. As we proceed eastward the strike becomes nearly N. and5.,
and the strata gradually assume a more gnarled, twisted appearance,
granite being visible here and there, Such highly metamorphosed
rocks continue to near the head of Loch Eil, where the micaceous
series is replaced by hard grey quartz-rock, first in highly twisted
and even vertical beds, with granite-veins. The dip then turns to
EK. 18° §, at 25°, exactly like the undulating quartz-rock of Glen-
garry ; after which the dip is reversed to W. 30° N. at 20°—25°.

About one mile east from the head of the loch we observed frag-
ments of red felspar in the streams. Two miles further on, the dip
was 8.E. at 20°-25°. At the distance of another mile the south-
easterly dip still continued, but at a very gentle angle.

One mile and a half east of Fassafern the hard grey quartzose beds
dip W. 25° N. at 17°-20°. Thence they undulate for four miles
along the margin of the loch. We next found them in well-marked
strata separated by layers of micaceous schist in a quarry by the
roadside, where they dipped nearly due W. at 25°-90°. ‘They are
traversed by innumerable veins of a pink felspathic rock; and larger
masses of a dark hornblendic rock are occasionally seen. Further
on the dip still continues westerly, and, at Avat, is at an angle of
from 25° to 30°. Four miles from Fort William another quarry
occurs close to the road, where hard grey quartz-rock, highly mica-
ceous in certain layers, and even passing into true mica-schist, dips
W. 16° N. at 30°-40°. The rock is traversed by veins of quartz
containing mica.

Near the church of Kilmallie the angle becomes much higher,
the N.W. dip still continuing. Beyond this we reach an area of
intense metamorphism, where porphyry and granite are intermingled
with the schists and quartz-rocks in great abundance along the
valley of the Caledonian Canal. This valley, moreover, is obscured
by enormous accumulations of sand and gravel.

The annexed diagram shows the arrangement of the strata along
the line just described. It will be seen that, viewing the country
on the large scale, we are here presented with a wide synclinal
trough of the schistose series, from beneath which, along either side,
the underlying quartzose rocks come to the surface,

3. Repetition of the Lower Silurian Quartz-rocks and Limestones
East of the Line of the Great Glen.

Line of Great Glen or Caledonian Canal.—We have shown that the
quartz-rocks and limestones of Sutherland range south-westwards

[ Feb. 6,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

206

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1861. | MURCHISON AND GEIKIE—HIGHLANDS. 207

through Ross-shire into the Isle of Skye,—that they are covered by
a vast series of micaceous flagey or gneissose schists,—that these
are disposed as a great synclinal trough, the centre of which tra-
verses the head of Glen Shiel, the middle of Loch Quoich, and the
watershed at Glen Finnan,—and that, by the curving of this trough,
the quartzose beds which form its outer or lower edge along the
western coast at Arisaig are brought up again along the line of the
Great Glen.

We shall now endeavour to describe the anticlinal arch of the
Great Glen, and to point out how the same strata undulate to the
eastward of that arch to form the remainder, or southern portion,
of the Scottish Highlands.

The remarkable chain of lakes which extends from Inverness to
Fort William presents, even on the roughest map, unmistakeable
evidence of a line of fracture in the earth’s crust. Loch Ness,
deeper by many fathoms than the German Ocean, showed, in the
sympathetic movement of its waters during the Lisbon earthquake,
the depth and extent of the fissure which it occupies. So marked a
line might justly be supposed to indicate a great displacement of the
rocks. And yet, though the fracture is probably more extensive than
any other in the country, it has not been attended, so far at least
as we have yet been able to ascertain, with any marked upheaval
or depression of the rocks on either side. We at present regard it
as a fracture without a throw, or, at least, with such a throw as not
at all to interfere with the regularity and perspicuity of the section.

The line of this chain of lakes, or the Great Glen, as it is properly
called, runs along the line of an anticlinal axis. West of the lakes
the strata (as we have seen along the banks of Loch Eil) have a
north-westerly dip; east of this line they incline to the south-east.
Moreover, it would seem that this axis lessens in intensity towards
the north and increases towards the south; in other words, the
southern prolongation of the arch brings up lower and lower beds,
while in its northern extension it appears to be dying away. As
we trace it southward from the grey quartzose beds last described at
Loch Fil, we gradually re-encounter the whole of the Sutherland
and Ross-shire succession of quartz-rocks and limestones, and ob-
tain thus additional aid in correlating the crystalline rocks of the
North-western Highlands with those of the central counties.

Islay and Jura.—By much the clearest and most complete series
of these repeated strata occurs in the Islands of Islay and Jura,
whence they range north-eastward up the Linnhe Loch, and south-
westward into Ireland. The annexed figure represents the struc-
ture of Islay (fig. 20).

The rocks which form the N.W. promontory of the island at
Sanaig were examined by us under the disadvantage of a storm of
wind and rain. We ascertained, however, that they consist of clay-
slate, which we believed to dip below the mica-schists and grit-
bands of Sanaig-farm. They are well exposed on the shore, first
with a south-east dip, which soon turns to the north-west, with
which inclination they appear to plunge below the waters of the

‘
208 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

Atlantic. The slate is cleaved obliquely to the bedding, the planes
having, where we saw them, a marked §.E. slope. This rock weathers
in a remarkable way along the precipitous headland of Sanaig. Seen
through the mist, the hills seemed split open by deep narrow fissures,
corresponding probably to joint-planes, while their steep faces had
that peculiar jagged aspect which so often results from the weathering
of cleavage and stratification combined.

If we are correct in assigning to these slates a position inferior to
the grits and schists which in Islay represent the lower quartz-rock
of Sutherland, it follows that they help to fill up a gap in the Silu-
rian series which is wanting in the North. The Sutherland rocks
unquestionably belong to the lower part of the Llandeilo series, and
the Sanaig slates would accordingly represent the position of the
Lingula-flags. ‘

The slates are followed towards the east by what we at present
regard as a superior series of schists and intercalated bands of
quartzose grit. From this point there is no doubt about the order
of succession. The strata dip towards the south-east,—the schists
occupying, as a rule, the valleys and low grounds, while the bands
of hard grit range along the island in more or less prominent ridges,
or even rising up into no inconsiderable hills. The schists do not
differ from those which have been already described; they. are
micaceous, chloritic, argillaceous. or quartzose in turn, and often
much contorted in their lamination. The grit or quartz-rock is a
hard grey siliceous rock, to which the old term “ grauwacke” might
well be applied. These strata occupy the whole of the western
division of Islay, known as “ the Rhinns,”—the schistose series being
sometimes quarried for slates, as at Kilchieran, and the grits as
rough building-stones. Granitoid rocks and true syenites are of
common occurrence, and may be advantageously examined along the
south-east side of the promontory at Port Charlotte. There, on the
shores of Loch-in-Daal, the quartzose grauwacke and grey schist,
dipping 8.E. at 40°, are traversed by a red syenite, and are them-
selves highly metamorphosed, passing into quartz-rock and lydian-
stone, in which a crystal of felspar may be occasionally detected.
The decomposition of the syenite here has produced that chaotic
assemblage of loose blocks (felsen-meer) so common in granitic
countries. Dykes of greenstone with a general north-west range,
but often irregular and tortuous, also occur among the strata of this
coast-line as well as throughout the entire island.

As we trace these schists and grits towards the N.E. promontory
of Islay, the former are seen to become considerably thinner, and the
series then assumes much more of a quartzose aspect. This was
particularly noticed on the high grounds to the north of Islay
House.

The section (fig. 20) shows that above the grits there is a series of
schists with three intercalated limestones. This upper series we
refer to the horizon of the Assynt limestone. It lies upon a quartzo-
schistose band, representing, as we have said, the lower quartz-rock
of Sutherland. Itis surmounted by a great mass of white quartz-

1861. ] MURCHISON AND GEIKIE—HIGHLANDS, 209

rock, the equivalent of the upper quartz-rock of the North, which is
overlain in both localities by an upper group of schists.

The lowest limestone is seen to the north-east of Islay House,
whence it runs for some miles towards the north-east in a broad
band. It is a grey crystalline rock, sometimes well bedded, and
exactly resembles portions of the Assynt rock. We could detect in
it no trace of fossils.

The space between this and the next limestone is probably occu-
pied for the most part by soft schists, as the country is low and
covered with peat. The second limestone resembles ,the first, but
appears to be of smaller dimensions.

After another interspace of moor, with here and there exposures
of schistose strata dipping towards the south-east, we encounter the
third limestone, which follows the curving outline of the escarpment
of quartz-rock and plunges sharply below it. This limestone, owing
to the form of the island, can be traced further than the others. It
extends from Lossit, near the shore of the Sound of Islay, to the
Mull of Oe, a distance of 16 or 18 miles. The cliff line at the latter
locality affords a good section of the junction of this calcareous seam
with the schists below and the strata of quartz-rock above it.

In tracing it northward along the western slopes of the mountains,
we find that it has a regular course until within a few yards of the
shore of the Sound of Islay near Lossit, where it suddenly wheels
round and passes towards the west. By this means it avoids enter-
ing the opposite island of Jura, and the superjacent quartz-rock is
thus thrown westward along the Islay shores instead of crossing at
once with a north-east strike into Jura.

The district between Lossit and Islay House presents a confused,
contorted arrangement of the rocks. The various limestones are no
longer separable ; they seem indeed to become blended more or less
into one, and on crossing the central valley towards the north they
die out altogether, so that the lower grauwacke-grits and the upper
quartz-rock unite. They are considerably mineralized, containing,
in at least one locality, veins of lead which are worked.

The upper limestone is surmounted by some schistose strata, well
seen at the Mull of Oe, which graduate upward into white quartz-
rock. The great mountain-masses of Beinn Bhan, Ben Vicker, and
other summits, looking in the distance as if capped with snow, consist
entirely of beds of this quartz-rock, having a south-easterly dip at
from 30° to 40°. Sometimes, however, the rock has a reddish hue
and a coarse granular texture, as along the cliff line of Macarthur’s
Head, where the strata have been considerably broken. Further to
the north it even assumes the character of a breccia, the included
fragments consisting of variously coloured felspathic rocks. The
upper beds of this quartzose mass descend rapidly towards the east,
and are succeeded by a group of schists (with intruded beds of
greenstone), which, in alternate ridge and valley, occupies the de-
scending ground between the grey mountain-chain and the eastern
shore*.

* Macculloch (Trans. Geol. Soe. vol. ii. p. 413) says, ‘‘ Extensive and correct

ow

210 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

The junction of the quartz-rock with these schists can be seen at
many places. Thus the sea has cut some instructive sections near
Macarthur’s Head, and still more clearly at the Mull of Oe. The
streams too which descend from the hills in an easterly direction have
laid open many exposures of the rocks. The junction-line of the
two series of strata is not a sharp one. The quartz-rock passes, by
intercalations of schist, into the schistose group, and the latter, by
interstratifications of quartz-rock, into the quartzose group. The
structure of this part of the island vividly recalls that of the east
coast of the peninsula of Sleat in Skye.

The schists which thus rest upon, and at their base are interlaced
with, the quartz-rock vary in character, being sometimes micaceous,
argillaceous, quartzose, chloritic, or taleose. These changes of litho-
logical distinction are so rapid that it is impossible to give any one
mineralogical name to the group, or to map out its ‘members by
mineral characters. Some of the argillaceous beds are quarried for
slate in Port Ellen Bay, where they have a rude cleavage. Some of
the harder beds of grit which occur among the schists have a green-
ish colour and a slightly chloritic composition, and (as at Port Ellen)
have been worked as building-stones. Sometimes the schists are
varied by the intercalation of hard micaceous and siliceous flagstones,
which are well exposed along the coast at Ardimersay, the residertce
of our very kind friend Mr. Ramsay of Kaldalton. One thin course
of limestone occurs at Kintore. z

But the most marked feature of this schistose series is the great
number and extent of its hornblendic greenstones. These are
grouped in long parallel ridges corresponding to the strike of the
strata. They are, however, beyond all doubt intrusive sheets, since
they alter the rocks along the line of contact, and do not always
conform to the bedding, but here and there cut across it, twisting
and hardening the surrounding schists*. The same sreenstones
occur also in the quartz-rock, but sparmgly. Their great develop-
ment is among the schists, where, along the coast from Port Ellen to
near Macarthur’s Head, they form the more prominent reefs and
islets, to which they give a narrow outline and a north-east and
south-west direction.

The whole of the Island of Islay is more or less traversed by a
series of basalt-dykes, which range in a general way from north-
irection which characterizes all the later
dykes of the western coast of Scotland. These igneous rocks cut
across every other rock in the island. Their posteriority to the
greenstones is beautifully shown on the coast south of Macarthur’s
Head, where the long crags of greenstone which run out to sea are
crossed by veins of basalt that pass from reef to reef with striking

observations on Isla would probably determine the true relative era of the
quartz-rock, and elucidate still further the disposition of Schihallien, of Jura,
and of the north of Scotland.”

* Since our observations were made, Mr. Jameson of Ellon has examined the
geology of the opposite mainland of Cantyre, and found that the schists there
are traversed by a similar series of intrusive beds of greenstone, which, as in
Islay and Jura, are crossed at right angles by a newer group of basalt-dykes.

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 211

persistence. These dykes may be seen high on the sides of the grey
quartz mountains, and one is especially observable a little below the
summit of Ben Vicker.

The Island of Jura, the magnificent mountain-ranges of which
form the deer-forest of our hospitable friend the Laird of Jura,
presents no feature which has not been already noticed in the
description of Islay. The limestones and lower schistose series are,
however, wanting; and the quartz-rock attains a much grander
development than in Islay, rising into the Paps of Jura, 2569 feet
above the sea. Macculloch has well described the singular and
striking view from the summits of these mountains, which altogether
constitute the grandest display of quartz-rock to be seen in Scot-
land*. Nothing can exceed the distinctness with which the lines
of bedding are impressed on the cliffs and along the ridges. The
whole island seems spread out as in a map, and we can follow
almost the line of each stratum as it winds over hill and crag,
valley and tarn, among solitudes that are haunted only by the red-
deer and the eagle. Here and there among the grey cliffs we detect

the dark line of a basalt-dyke pursuing the even tenor of its way to- —

wards the north-west, alike over precipitous mountain and deep glen.

The line of schists which fringe the eastern coast of the island
correspond to those that occupy the same part of Islay. They are
marked too by the same lines of greenstone, ranging into the beds,
and are traversed by the same series of later basalt-dykes.

Prolongation of the Islay and Jura Rocks up the Linnhe Loch.—
The limestones of Islay, overlain, as we have shown, by a great
quartz-rock series, are prolonged towards the north-east in the Gar-
velloch Isles and the Islands of Lismore and Shuna. The quartz-
rock above them, after traversing the length of Jura and Scarba,
becomes lost beneath the sea. But we find traces of it again, though
in a greatly diminished form, along the eastern shores of the Linnhe
Loch, north of Oban. It there occurs as bands of quartz-rock and
quartzose flaggy beds among schists, and dips, lke the limestones
below and the schists above, towards the south-east. The upper
schistose series, with its associated limestone bands, skirts the eastern
shores of Jura and Scarba, and thence runs towards the north-east,
forming, with the addition of later rocks, the chain of islands towards
Oban as well as a large part of the mainland.

The crystalline series of strata, therefore, which is so clearly ex-
hibited in Islay, is continued up the Linnhe Loch, the rocks having a
steady south-easterly inclination. This line forms one side of the
anticlinal arch which has been pointed out as coincident with the
direction of the Great Glen, or line of the Caledonian Canal; the
other side is lost beneath the Atlantic. In the reverse or north-

* Description of Western Islands, vol. ii. p. 205, &c. See also Trans. Geol. Soc.
vol. ii., where he gives other details. His section of the order of superposition
agrees with our own. He says that the quartz-rock of Jura underlies the slates,
and contains water-worn pebbles, also worm-like cylindrical borings, and that it
was “originally a stratified sandstone which has been chemically and me-
chanically altered.” (pp. 454, 455, 462-3.)

owe pf

212 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

westerly dip of the slates at Sanaig Point in
} Islay, however, we see the beginning of the
curve, which is doubtless continued towards
the north-east until it joins the line of section
already described at Loch Kil.

One or two localities along the north-eastern
prolongation of the Islay series were examined
by us in detail, and present features of sufti-
cient importance to merit separate notice.

Seil and Easdale.-—These islands consist
fundamentally of clay-slate belonging to the
upper schistose series, and lying on the same
general horizon with the schists and slates
which range along the eastern shores of Islay
and Jura. The slates have a general south-
easterly dip, and range into Lorn, but are
there buried beneath a mass of later igneous
rocks, and partly also under a series of reddish
sandstones and conglomerates.

Kasdale consists entirely of slate, with the
exception of certain N.W. and S8.E. green-
stone-dykes. Seil presents a greater variety :
its north-western half consists of an outlier of
the Lorn trap, resting, apparently conform-
ably, on some sandy conglomerates which lie
in complete unconformity on the slates.
These conglomerates form part of the same
series which in Lorn, as around Oban and
along Loch Feochan, underlie the igneous
rocks and cover over the slates unconform-
ably.

The annexed section, fig. 21, explaims the
structure of this island. Without cumbering
the present memoir with details, it may be
enough to remark that the slates vary in dip
from 8. 40° E. to 8. 64° E., and the angle from
25° to 82°. In a line passing a little north-
west of Kilbrandon Church, and reaching
the north-east shore near some old slate-
quarries, there appears to be a slight fold ;
but, with this exception, no stance was met
with of an inclination to north-west. The
south-east limb of the island has a strongly
marked ridge running parallel to the strike of the strata. It ex-
actly resembles the ridges along the eastern flank of the Islay moun-
tains, and consists, like them, of a magnesian greenstone which
has been intruded parallel to the bedding. This rock is traversed
here, as in Islay and Jura, by transverse N.W. and §.E. dykes of
greenstone or basalt. These dykes also cut through the conglome-
rates as well as the sheet of greenstone to the north-west. They

8.E.

* Dykes of Basalt.

WN S
SSS

SSS

a

Length 41 miles.

xx Amygdaloidal Greenstone.

Fig. 21.—Section of the Island of Seil.
t Greenstone.

e. Conglomerate.

*
d. Clay-slate.

1861.] MURCHISON AND GEIKIE—HIGHLANDS, 213

occur abundantly, too, on the opposite island of Easdale, where they
present some interesting features in relation to the different rates at
which the various parts of the dykes cooled.

The slates of Easdale and Seil present perhaps the most perfect
cleavage yet known in Scotland. The cleavage-planes lie in the
same direction as the bedding—that is, towards the south-east—but
generally at a higher angle. The following list of observations, taken
from Easdale, across the strike of the Seil slates, will show the ratio
of the two planes :—

Easdale (south side): slates dip S. 62° H. at 32° ; cleavage same direction at as

” ” ” S. 46° E. at 25° ; ” ”
xs 96 5 S. 64° BH. at 68°; 3 ne 42°.
Seil Harbour is 8. 54° E. at 82°; ai a Dogs
» (west shore) ‘ 8. 45° E. at 27°; Fe 43 55°.
5 . is 8. 40° E. at 33°; as Bs 57°.
9 . re S. 52° BE. at 27°; PiEMS aoe EB. 42°.
» (1 mile N.W. of Kirk) S. 60° E. at 60°-67°; ,, 60°-70°.
. (old slate-quarries) __,, obscure dip ; 5 8. 66° BE. 27°-45°.
», (100 yds. N. of last obs.) 8S. 60° E. 60°-70° ; » 8. 66° FB. 40°.
, (eastern shore) 3 8. 56° H. 25°; SOOM E. 62°.

The bedding of the slates is distinctly defined both by lines of
colour and by the intercalation of seams of hard blue sandy mud-
stone, nodules of which also occur in theslate. The cleavage is most
perfect where the slate is finest in grain ; some of the sandy beds are
only rudely cleaved, and others show no cleavage at all. The sur-
faces of the cleavage-planes are finely waved or foliated, and contain
numerous cubes of iron-pyrites.

Eastern Shores of Linnhe Loch.—The slates of Seil and Easdale
are soon lost in their northward prolongation under the sheets of
greenstone and underlying reddish sandstones* that form so large a
tract in Lorn. North of Oban, however, we find the quartz-rock or
quartzose flagstones rising in terraces along the east coast of Loch
Linnhe, especially in the neighbourhood of Port Appin. They are
covered by the upper limestones and schists as in Islay, and are
clearly underlain by the thick limestone of Lismore. The section
at this place therefore forms the counterpart of that of Islay to the
south, and that of Ross and Sutherland to the north.

Glen Spean.—The same order of succession continues up the Great
Glen, which, as we have already shown, coincides with the line of an
antichnal axis. The quartzose strata which have been described as
occurring at the head of Loch Eil, and thence eastwards to Banavie,
roll over to the south-east, and are followed by schistose beds con-
taining several seams of limestone. The stream in Glen Spean, on
the north side of Ben Nevis, shows the succession well. At the
Bridge of Spean, quartzose and schistose strata dip 8. 55° E. at.a
high angle. Quarter of a mile to the eastward, quartzose flagstones,
much altered, with intercalations of bluish-grey micaceous and talcose
schist, dip 8. 62° E. at 65° to 90°. This same quartzose series con-

* The thick-bedded, very hard, greenish, siliceous sandstone on Loch Feochan,
south of Oban, is undistinguishable from many portions of the Old Red Sand-
stone, but may be of later age.

VOL, XVIJ,—PART I, @

214 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

tinues up the glen for about a mile in nearly vertical beds, striking
N. 16°-24° E., with a slight inclination to the south of east. The
beds are flaggy and micaceous, and sometimes so pulverulent that
they might be called sandstones. They are succeeded by a set of
flagey, very micaceous schists, nearly vertical, sometimes quite so,
striking N. 44° E. Here a series of bands of grey crystalline lime-
stone occurs, with the lines of stratification well marked, especially
where layers of schist 1 to 4 feet broad are intercalated with them.
A little higher up the river some dykes of felspathic and hornblendie
greenstone occur, striking with the strata N. 34° E.

The same schists continue up the valley, though greatly obscured
by deep drift. They are sometimes talcose, sometimes strongly
quartzose, but usually micaceous. At the Bridge of Roy they strike
N. 45° E. with a south-easterly dip of from 60°-80°.

Here again therefore we are presented, along another line of sec-
tion, with the same order of superposition. Quartzose strata, cor-
responding to the upper quartzose flaggy series of Sutherland and
Ross and the upper quartz-rock of Islay, pass up into a set of schists
which in their lower part contain calcareous seams, exactly as in
Sutherland, Ross, and Islay.

Loch Leven.—Between the section just described and that of Port
Appin above alluded to, there is an excellent transverse exposure of
the rocks along the shores of the maritime Loch Leven. In skirting
the east side of Loch Eil from Fort William southward, the passage-
beds, so to speak, between the quartzose and the schistose series are
seen on the road-side much contorted and broken, but with a
general northerly strike and easterly dip. As we approach Loch
Leven, thick bands of white quartz-rock are seen to occur in the
series ; and on reaching the margin of that loch we find the whole
plunging sharply to the south-east. A bed of limestone is quarried
here, above which lies a thick band of white quartz-rock, and then
come the true slates of Ballahulish, which lie on the same horizon
with those of Easdale.

The intercalation of white quartz-rock above the limestone and
the general interlacing of the quartzose and the schistose series are
facts of great importance.

On the south side of Loch Leven the same slates are well exposed.
In spite of the granite and porphyry masses which here occur, they
have a marked north-easterly strike, and where first seen, though
nearly vertical, incline towards the south-east. Gradually they be-
come vertical; and then, among the great slate-quarries, they take a
high westerly dip. They are traversed by a cleavage very inferior
to that of Easdale, and apparently in the quarries coincident with
the lines of bedding. A little eastward, however, on the side of
the high road, beyond an archway, there is a good section of the
slates, which dip 6°-10° 8. of W. at 45°. They are traversed by
cleayage-planes which dip in nearly the same direction at 75°. These
planes cut through alternate beds, the coarser sandy layers being
uncleaved. Immediately under the slates comes a thick band of
hard blue and grey compact and flinty limestone, with lighter bands

1861.] MURCHISON AND GEIKIE—HIGHLANDS, 215

interstratified through its mass. In its upper part it dips 12° S. of
W. at about 75° with a rude oblique cleavage. Mastwards the dip
changes to nearly S.W., and the angle varies from 50° to 70°. The
limestone, with slaty interstratifications, continues to occupy the
shore for at least half a mile, when it is underlain by another
series of slates and schistose beds towards the entrance into Glen Coe.

Glen Coe.—As we ascend this glen the slates are succeeded by
quartzose rocks, and the whole valley is traversed by a network of
bands of porphyry. The quartzose strata, however, appear to have a
decided westerly or north-westerly dip, which towards the entrance
of the Pass of Glen Coe becomes very gentle and then undulates
to the S.E. The amount of alteration now becomes very great.
Dykes and masses of felspathic porphyry abound, and it becomes
difficult to detect the actual bedding of the strata, which are split
vertically by a kind of jointing or rude cleavage. Towards the head
of the Pass the schists or slates are again met with, but in an in-
tensely altered condition, having passed into lydian-stone or jasper.
In spite of this metamorphism, however, we believed that they
showed a 8.E. dip. ‘Towards King’s House masses of granite occur 3
and the whole of this region, extending eastwards over the wild
moor of Rannoch and southwards among the mountains of Cruachan
Ben, is eminently metamorphic.

The Breadalbane Forest.—The metamorphic region just alluded
to forms part of the great deer-forest of the Marquis of Breadal-
bane, and is a good centre from which to explore the geology of this
part of the Scottish Highlands. A reference to previous geological
maps will show that this extensive tract has been coloured as
* pneiss” with large areas of granite. In truth, however, the region
is not one of true gneiss; nor, so far as we observed, does the gra-
nite occur in the large, well-defined areas which have been assigned
to it. On the contrary, the same lower quartzose series and upper
schistose series form the groundwork here, as in such vast areas of
other parts of the Highlands, granite and porphyry occurring abun-
dantly in veins, knobs, hillocks, hills—in short, in every variety of
form and size, across the belt of country from Ben Cruachan to Loch
Rannoch, North-west of that belt, that is, along the Loch Leven
shores and towards Glen Coe, the order of succession is plain ;—
south-eastward through Glen Orchy and the surrounding country,
as we shall immediately see, the order is equally clear; and even
in the granitified tract itself we are at no loss to determine along
what part of the great Lower Silurian series it lies. There is no
trace of any protrusion of the lower or Laurentian gneiss. The
stratified rocks indeed, as was pointed out to us on the spot by
the noble proprietor, are occasionally hornblendic; but they cannot
properly be called gneiss, nor can they for an instant be mistaken
for the older gneiss of the North-western Highlands and Islands.

The Moor of Rannoch* may be regarded as an undulating dome

* Macculloch (Trans. Geol. Soc., old ser., vol. iii. p. 129) describes the Moor
of Rannoch as a rugged plateau of granite, which extends to the head of Loch

Rannoch, or for twenty-four miles, and as ‘‘one of the most complicated and.
Q2

216 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

of the quartzose rocks, with here and there perhaps, where the un-
dulations are broader and deeper, an outlier or basin of the schistose
series. At the Bridge of Bah, between King’s House and Inverouran,
the quartzose flagstones have a N.W. dip, and rise from under the
highly altered schists of Glen Coe already referred to. The dip va-
ries greatly even at short distances, but from this point towards the
south-east the north-westerly direction is on the whole maintained.
It is well seen at Loch Tulla, near the Marquis of Breadalbane’s
Shooting Lodge of the Black Mount, and on the opposite mountains
of Ben Or, Ben Doran, Ben Do, Ben-na-chalader, and Ben Chrechan.
The south-easterly dip is resumed at the watershed, and eventually
towards Tyndrum we return again upon the schists.

Before entering into the details of the eastern side of this great
anticlinal arch, we here give the results of an excursion by Glen
Orchy to Dalmally, and thence to Cruachan, whereby one of us
defined the southward limit of the arch, whilst the other explored,
for the third time, from the hospitable centre of the Black Mount.

Black Mount by Glen Orchy to Loch Awe.—The quartzose flag-
stones of Loch Tulla are well seen in the channel of the stream
where the road crosses the Orchy. ‘They dip N. 36° W. at 15°-25°.
They are micaceous, the mica being especially abundant along the
planes of bedding, whereby a fissility is given to the rocks. About
a quarter of a mile below the bridge the same quartzose micaceous
strata turn round to due N., but a short way down they resume their
dip to N. 26° W. at 20°-30°. Here they are well-marked flag-
stones, each flag being separated from its neighbours by plates of
silyery mica. As we descend the stream the character of the rock
continues the same for several miles, but the dip gradually veers
round to W., W. by 8., and 8.W., at the same gentle inclination: by
this change the series is slowly repeated; and the beds eventually
becoming more and more micaceous, are, in fact, in many places true
mica-schist. At Achenafanich, near the bottom of Glen Orchy, a band
of white quartz-rock is seen descending obliquely the west side of
the valley with a south-westerly dip. It is clearly underlain by
some darker micaceous beds and covered by others of a similar
kind. At the bottom of the glen, where the two roads meet, schistose
micaceous strata dip W. by 8. at 25° or 30°. They are traversed by
a dyke of augitic greenstone, which runs W. 10° N., rises along the
hillside to the north of the Orchy, and crosses the valley at the head
of Loch Awe near Stronmelch. In Professor Nicol’s Map this dyke
is marked as having a N.N.E. strike. A parallel ridge to the south
may possibly mark the line of another dyke, but we did not examine
it. About a mile and a half before reaching Dalmally some flaggy
schistose beds are seen in a brook by the roadside, dipping 8. by W.

In the streamlet close to the inn of: Dalmally, fissile mica-schist
dips 8. 16° W. at 55°; and a short way further west, in an old quarry,

interesting districts in the whole range of Scottish geology.” This granite extends
south-westwars into the shoulders of the mountains to the south of the King’s
House, where it was pointed out to us by Lord Breadalbane in the old military
road of Marshal Wade, and where it is not marked in previous maps.

13861. | MURCHISON AND GEIKIE—HIGHLANDS. 217

the strata are highly argillaceous as well as micaceous, dipping 8. 50°
W. at 42°. At the manse a seam of limestone was formerly quarried.
Where the road crosses the Orchy, sandy micaceous schist dips §. 66°
W. at 45° to 55°. The same south-westerly inclination continues
towards the head of Loch Awe. Beyond Stronmelch, the greenstone
dyke already described descends from the hillside and plunges below
a drift-covered peaty plam. ‘The strata at the head of Loch Awe
seem to be greatly contorted, having in places even a north-westerly
dip. Another dyke of greenstone, possibly a prolongation of the second
ridge at the foot of Glen Orchy, which we conjectured to consist of
greenstone, crosses the road on the west side of the Loch Awe valley
a short way south of the point where the road crosses the Main
Water. Quarter of a mile from the bridge a streamlet has laid open
a good section of some quartzose flagstones, micaceous and chloritic,
dipping S. 52° W. at 35° to 40°.

We made copious notes of the section along the western shore of
Loch Awe to the outlet of the river, but we need only cite here one
or two of the more important facts. The dip, sometimes reversed
and frequently varying, maintains on the whole a south-westerly
direction, and the strata become very schistose as we ascend in the
series. Mica, chlorite, and tale are the distinguishing minerals.
About seven miles from Dalmally a bed of hard siliceous limestone
occurs, with occasionally a green serpentine colour, and many thin
talcose seams. It also contains lenticular masses of white quartz,
and dips 8. 54° W. at 48°. Above this limestone come several
other bands of a similar rock, forming as a whole a thick limestone
series. Serpentine abounds, giving the beds a green colour. Felspar-
perphyry is also abundant, both in the form of beds parallel to the
planes of stratification, and also as veins cutting through the strata
irregularly. This porphyry deserves remark. Where disposed in a
bedded form, it is traversed by lines of quartz corresponding exactly
to the lines of bedding of the adjacent limestones and schists. It
contains much tale, which, however, is invisible in the cross fracture,
but shows a silvery surface along lines parallel to the bedding-planes.
Otherwise the rock appears to consist mainly of pink felspar. The
aspect of these porphyries more than once suggested the idea that they
were only more highly mineralized portions of the stratified series
that had been metamorphosed tn situ.

The schists with innumerable dykes and veins continue down the
Pass of Loch Awe. They appear eventually to be reversed to S.E.,
showing thus the commencement of the other side of the trough
which begins with the south-westerly dip of the strata in Glen
Orchy. The granitic region of Cruachan Ben intervenes between
the Awe and Loch Leven, rendering a careful examination necessary
before the geological lines at these places can be safely joined. In
the meantime, howeyer, we regard the synclinal trough of Balla-
hulish as a continuation of that of the Awe—an inference which
the general strike of the strata at both localities and over part of
the intermediate ground seems to render probable.

Dalmally to Tyndrum.—the section up the glen from Dalmally

218 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

to Tyndrum is very instructive. The dyke which has been already
noticed as trending in a W.N.W. direction from the head of Loch
Awe to the foot of Glen Orchy, runs along the northern side of
this glen for about five miles from Dalmally, beyond which we
failed to trace it. The schistose rocks, seen where the two roads join,
are succeeded by inferior beds of quartzose flagstones, often highly
micaceous. These gradually change their dip from 8.W. to 8., and
to 8. by E. and 8.E. The angle of inclination is gentle (15°-20°),
so that the same beds which occur at the top of the hillside on one
side of the glen are seen at a lower level on the other, the 8.E. side
being steeper, since it is the escarpment, and the north-west side
more shelving, the slope often nearly coinciding with the dip of the
strata. As we ascend, the oblique direction of the glen brings us
across the strata in a gradually ascending progression until we arrive
again at the micaceous schists. These are seen in the streams around
Tyndrum, where they have a marked 8.E. dip.

From this section it is evident that the anticlinal arch of the
Breadalbane Forest sinks down towards the south below the schists,
which curve round the quartzose series in a wide semicircular sweep
that extends from the flanks of Cruachan by Dalmally to Tyndrum.

The Black Mount to Tyndrum.—The quartzose flagstones of Loch
Tulla ascending into the Ben-Do range have there a marked north-
westerly dip, with a gentle inclination of 10° or 15°. Ascending by
the road from Orchy Bridge we find the flaggy beds well exposed in
rayines and cuttings by the wayside. The north-westerly dip and
gentle angle continue until towards the watershed, when the beds
begin to incline to the north, then gradually to the north-east and
east, until, when the summit of the road is reached, they take a de-
cided south-easterly dip, and a higher angle than on the north-
western side. By this means the flaggy beds are repeated, and we
speedily pass into the schists that overlie them.

The axis of the Ben-Do and Ben-na-chalader chain strikes to-
wards the north-east into the Brae Lyon mountains. It is, however,
only a minor anticlinal fold along the great arch of quartzose rocks,
which we have defined as ranging through the Breadalbane Forest
from Ben Cruachan to Glen Rannoch, beyond which it stretches
away into Atholl Forest and the heart of the Grampian Mountains.

It remains now to describe the disposition of the schists as they
fold round the south-eastern side of this great arch.

Tyndrum to Loch Tay.—F rom Tyndrum down Glen Dochart the
schists have a south-easterly dip at from 10° to 15°. They occa-
sionally become highly altered, however, with a more rapid dip.
About a mile N.W. from Crianlarich, limestone is quarried. It is a
hard, blue, crystalline and fissile limestone with numerous green ser-
pentinous and talcose interlaminations, as at Loch Awe*.

At Loch Dochart the schistose or gneissose strata are much gnarled
and twisted, dipping in various directions from N.E. toS$.E. The
whole of the valley of the Dochart is more or less obscured by drift,

* See this limestone described by David Forbes, Quart. Journ. Geol. Soc.
rol. xi. p. 166.

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 219

and the rocks are consequently for long distances obscured. As we
approach Luib the dip appears on the whole north-easterly. There
the beds seem undulating along an H.N.E. axis ; but they may pos-
sibly be reversed to N.W. Near Luib we saw no rock decidedly in
place; but some exposed ledges appeared to have a N.W. dip.

To the north-east of Luib, limestone has been worked on both
sides of the glen. The seam appears to run along the north-west
“side, and is at present quarried on the declivity a short way west of
Killin. Below the limestone in the bed of the river, flagstones are
seen nearly horizontal, evidently the beginning of the quartzose series.

Thus from Tyndrum to Killin we cross obliquely a synclinal
trough of the schists with limestone at either side, below which lie
the quartzose flagstones. This trough extends north-eastward by
Ben Lawers and Strath Tummel to the head of Glenshee, whence it
appears to enter the Grampians. To the south-east it is prolonged
by the head of Loch Fyne to the Atlantic at Loch Swene.

Loch Tay*.—This magnificent sheet of water occupies the line
of another anticlinal arch. The limestone just referred to as occur-
ring to the west of Killin, sweeps along the north-west side of the
lake, and plunges below Ben Lawers. In reality there are several
limestones here, as there are at Loch Awe; but we did not stay
to note the details, being satisfied that the whole formed a calca-
reous group above the flagstones and below the schists. On the
south-east side of Loch Tay the limestones also occur, having a
south-easterly dip, and passing under the schists, which here, as at
Tyndrum, contain the well-known metalliferous veins worked by the
Marquis of Breadalbaner.

We are not aware -how far the limestones stretch towards the
south-west. Those of Loch-Harn-Head appear to belong to another
arch. Towards the north-east of Loch Tay they are soon lost, but
reappear in the valley of the Tummel at Pitlochrie.

The numerous sections along the side of Loch Tay afford ample
scope for working out the details of this region. There is no more
beautiful district in Scotland, nor, at the same time, one where the
geologist might better acquaint himself with the order of super-
position, lithological characters, and mineralogical riches of the
younger portion of the crystalline rocks of the Highlands.

Loch Tay to Glen Lyon.—This traverse of the mountain-ridge of
Ben Lawers need not be detailed. It shows the limestones of Loch
Tay plunging below the schists of the ridge, which are often crumpled
and contorted. On the north-west side the dip changes to south-

* Tt gives us great satisfaction to state that before entering upon our labours
of the last summer, Professor Harkness had the kindness to furnish us with
coloured sections made by him during an earlier part of the same year, of part
of the country to the south-east of the line of the Caledonian Canal. His re-
searches were, we found, in complete harmony with our own; and his section of
Ben Lawers especially was of great use to us. He has since further extended
his observations into the North of Ireland, and found there the same order of
succession among the crystalline rocks, as will shortly appear in a paper com-
municated by him to the Society.

+ See Quart. Jown. Geol. Soe. vol. xvi. p. 421, &e.

220 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

east, and the crumpled schists are repeated, until at Glen Lyon the
limestone emerges from below them, followed in its turn, as usual,
by the quartz-rock. Thus the enormous mass of Ben Lawers, like
many other mountains in Scotland, as well as elsewhere, actually
occupies a synclinal trough, while the deep valley of Loch Tay, lke
that of the Great Glen, runs along an anticlinal arch.

Loch Tay to Loch Rannoch——The mountainous road from Ken-
more, by the north-east flank of Schiehallien to Loch Rannoch,
affords a cross section of the upper schistose beds in their prolonga-
tion along the synclinal axis of Ben Lawers, with the limestone
below them and the underlying quartz-rock, to perhaps a greater
depth than any other locality in the Central Highlands, The north-
west dip of the schists continues for some miles beyond Kenmore.
At the waterfall close to the road, north of where it crosses the River
Lyon, the dip is N. 16° to 30° W. About a mile south of the White-
bridge toll-gate the dip changes again to S.E., forming thus the
north-western side of the trough. As we proceed, we find the lime-
stone rising again in great force from under the schists. It is quar-
ried at the end of Loch Kinardochy, where it resembles the Loch
Tay limestones, but is greatly contorted. We believe that from this
point it ranges across Strath Tummel, and joins the great limestone
series of Blair-Atholl, with which it is undoubtedly identical.
Following that branch of the road which strikes to the left towards.
Rannoch, we come to grey micaceous flagstones dipping 8. 26° E. at
from 55° to nearly 90°. Veins of a red felspar-porphyry are not
unfrequent. About four miles from Loch Rannoch, after passing
over a great thickness of quartzo-micaceous flagstones, the road
enters a thick zone of limestone, which when first seen is covered
by dark silky schists, and hasa8.E. dip. It soon rolls over, how-
ever, and appears to undulate, often in sharp folds, for a long way,
after which the ground becomes obscured by drift until Kinloch
Rannoch is reached.

The section along the north side of the valley eastward from
Kinloch Rannoch shows that quartz-rock, sometimes as thick-
bedded and brilliantly white as that of Sutherland or of Jura, some-
times flagey and micaceous, underlies the hmestone. Near the inn,
the flagstones dip E. at 55°, and are probably intermingled with
syenite, large blocks of which strew the hillside. At Drumihastle
the limestone occurs again, having crossed the valley of the Rannoch,
and it here dips E. 8° N. at 65°. It is flaggy and finely laminated,
and is associated with dark schists, as on the south side. Above the
limestone, white quartz-rock and flaggy beds supervene.

The subjoined figure represents the section from Loch Kinar-
dochy to Loch Rannoch. It will be seen that the limestone at the
former locality les below schists, and, as we have seen, represents
the calcareous bands between the schists and the quartzose series on
Loch Tay, and indeed throughout the whole Highland region. Be-
low this limestone come the usual quartzose strata. These form
the higher part of the giant Peak of Schiehallien. But they are here
underlain by a thick limestone, and that by another quartz-rock

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 221

group—a much more complete series than appears to occur any-
where else east of the line of the Caledonian Canal.

Fig. 22.—Section of Schiehallicn, Perthshire.
N.W. Schiehallien. S.E,

Loch

Loch
Kinardochy.

Rannoch.

Quartz-rock with some schist and a bed of limestone. Schists and a bed
of limestone.

At the time when our observations were made, we believed that
in this second limestone we had found the prolongation of the great
lower calcareous zone which in Sutherland and Ross, as well as far
to the southward, in Islay, subdivides the quartzose group into an
upper and an under series. ‘The extension of our survey to the
north and to the east served to confirm this inference. We found
the limestone as it stretched northward become thinner, until, not
far beyond Glen Erochie Inn (above which, on the north side of the
valley, it has been worked), it appears to die away altogether; and
it does not occur in the consecutive section along the channel of the
River Garry.

Here, then, along the great anticlinal axis of the Breadalbane
Forest already described, there is a lower part of the series brought
up than at any other locality throughout this tract. It is important
to remark, too, that the greater extent of the curve only serves to
bring up strata already known in other districts, and which could
have been confidently predicted to exist here, as soon as it had been
ascertained that there occurred a lower set of beds than the flag-
stones of the Black Mount. Thus confirmatory evidence is obtained
of the correctness of the present explication of the order of succession
throughout the Central Highlands.

Dalnacardoch to Blair*.—As the road winds over the hills from
Glen Ercchie to Dalnacardoch, a marked dyke of porphyritic felstone
with hornblende strikes through the limestone and the micaceous
flagstones in a nearly north and south direction, and runs for a long
way northward. It occurs again in the bed of the Garry, at Dalna-
eardoch Inn, and on the hill above the road, with a breadth of 15 or
20 feet and a strike from §.8.W. to N.N.E. How much further
north it extends we did not ascertain.

There is an admirable section of the quartzose series along the bed

* This tract, according to Macculloch (Trans. Geol. Soc. Ist series, vol. ii.
p- 297), is wholly, or in great measure, composed of hard argillaceous schist, gra-
duating into argillaceous quartz-rock, and more rarely into mica-schist, with
granite-veins here and there dispersed through it.

222 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

of the River Garry, both above and below Dalnacardoch. Above the
inn, the quartz-rock, in well-bedded fissile flagstones, dips to the 8.E.
at an average angle of 30° to 35°. Several small dykes of felspar-
porphyry, running along the strike of the beds, occur about three-
quarters of a mile to the north-west of Dalnacardoch. The south-
easterly dip continues for three miles up the Garry, though towards
the end of that distance it becomes subject to undulations, showing
that the strata are on the eve of turning over in an opposite direc-
tion. This reversed or N.W. dip is well seen in the channel of a
torrent on the right-hand side of the glen, about three miles north
of Dalnacardoch. There, grey flaggy quartz-rock dips N. 42° W.
at about 30°. The stream has brought down an immense quantity
of shingle from the hillsides, chiefly of grey quartz-rock, with not a
few fragments of reddish felspar-porphyry. Above this, the bottom
of the valley is drifty and alluvial; but the colour and form of
the bounding mountains left us in no doubt that the same quartzose
series extends northward beyond the Pass of Drummuchter.

The descent of the Garry from Dalnacardoch exhibits a clear
ascending section of quartzose flagstones, occasionally schistose and .
micaceous. The dip is as nearly as may be 8.E., and the angle
ranges from 25° to 60° or 70°. Even allowing for some reduplica-
tions, the thickness of this series must be very great. Here and
there, as at 53, 42, and 4} miles respectively from Blair, dykes and
masses of felspar-porphyry occur, with a general strike from N. by E.
to 8. by W. ‘Two miles and a half from Blair the series is terminated
by the superposition of a very thick limestone series.

Blair-Atholl and Glen Tilt-—In following out the curvatures and
breaks of the rock-masses and their reappearances in a regular se-
quence as we proceeded from the north-west to the south-east, it was
evident, from proofs of superposition only, that when we came to the
south-western flank of the Grampians we had once more reached the
upper crystalline series. On a former occasion a similar ascending
succession to the younger stratified crystalline schists, whether mi-
caceous, quartzose, or chloritic, with bands of gneissic character and
argillaceous slates, had been traced from the heart of Ross and Inver-
ness to the northern, eastern, and south-eastern flanks of the Gram-
plans, as seen in the counties of Moray, Banff, Aberdeen, Kincardine,
and Forfar*. To the last of these tracts we shall presently advert.

In examining the south-western flanks of the Grampian chain
near Blair-Atholl, it was indeed quite manifest, judging even from
the flaggy and schistose characters of the rocks, that we were already
among strata superior at all events to the lower quartz-rock and
limestones of the north-west. Glossy shillat with micaceous schists,
resting upon granular quartz-rocks and limestones, and even alter-
nating with them, presented to the eye a mineral development un-
known in the lower members of the altered Silurian rocks of the
North-west, and wholly unlike anything in the Cambrian rocks and
fundamental gneiss of the outer Hebrides and the west coast of
Sutherland.

* Quart. Journ. Geol. Soc. vol. xv. p. 389 ef seg., and vol. xvi. p. 237, &.

1861. | MURCHISON AND GEIKIE—HIGHLANDS. 223

We were now upon the ground rendered classic by the researches
of Hutton, Playfair, and Webb Seymour, in which, with the memoir
of the last-mentioned of these eminent men in hand, we had only to
admire the truthfulness of their descriptions *, which show, even
down to the minutest details, the infinite ruptures of such strata,
their divergent directions, and their varied phases of metamorphism,
when in contact with or in the proximity of the syenites and green-
stones of the region.

In fact, Playfair and his associate Lord Webb Seymour had here
collected specimens which in one and the same escarpment on the
left bank of the Tilt (not exceeding 600 feet in height) offered proofs
that granular limestone and quartz-rock were surmounted by mica-
slate and gneiss, the latter again alternating with thin quartzose
bands. The great variety of compound rocks detected by these close-
searching explorers, from a small area on the banks of the Tilt and
its affluents, at once demonstrated to us that along the flanks of the
Grampians there exists a richness and variety of mineral develop-
ment which is unknown in the oldest members of the series to the
north-west. Thus, Lord Webb Seymour cites many compounds of
quartz, mica, felspar, hornblende, actinolite, compact dolomiter, tale,
steatite, and serpentine, mixed in a great variety of combinations
and in different proportions ¢.

In the same tract of Glen Tilt we saw cause and effect admirably
displayed, as pointed out by Hutton, Playfair, and Seymour. With
bosses of granite, syenite, and porphyry at hand (mere spurs, however,
of the gigantic granitic and porphyritic masses of the Grampians) we
at once understood how some of these younger crystalline strata
had been converted into the gneiss of the above-mentioned authors,
and had become associated here and there with granular quartz-
rock and limestone, in which the signs of their having been ori-
ginally sandstones and calcareous mudstones could not be doubted.

The numerous disruptions in the tract east of Blair-Atholl have
thrown the strata into a multitude of fragments, as will be best
understood by referring to Lord Webb Seymour’s diagrams, and
particularly to plate 20 of his Memoir, in which upwards of forty
cases of the strike $ and dip of the beds are given. Whilst most

* Not having with us the memoir of Lord Webb Seymour, we were indebted
to the Duchess of Atholl for the loan of it; whilst the Duke laid open to us the
recesses of Glen Tilt by giving us as our guide his head-forester.

t Lord Webb Seymour notes that compact dolomite is found in Glenelg and
Kintail. We also found there so much actinolite as to form, in fact, actinolite-
schist, with much talcose schist as well as granular limestone. It will therefore
be seen that the superior position we have assigned to the rocks of Kintail,
Loch-alsh, and Glenelg is borne out by their mineral characters also and their
similarity to the rocks of Glen Tilt.

t Trans. Roy. Soc. Edinburgh, vol. vii. p. 317.

§ The word ‘stretch’ has been used by these eminent Scottish geologists to
signify the direction as at right angles to the dip of the strata; and we almost
regret that, unmindiul of the earlier employment of this appropriate term, one
of us, in unison with Professor Sedgwick, was the first to recommend the
adoption of the word strike, from the German “Streichen” of German geolo-
gists. See Trans. Geol. Soc., 2nd series, vol. iii. p. 3877 (note).

224 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

of these masses preserve the normal strike of N.K. and 8.W., with
considerable deviations, however, to the N. and 8. of E., there are
examples of east and west directions; and we meet with others
(particularly high up the Tilt, between the Clochan and the Tarff)
where the strata striking from 8.E. to N.W. are there placed at
right angles to the direction of the normal masses. This takes place
where intervening syenitic and granitic rocks occur, the stratified
rocks being arranged with divergent strikes and dip around such
amorphous bosses.

In fact, it is sufficient to ascend the Banavie Burn from the Castle
of Blair for half a mile to see every possible discordant break among
strata of limestones and schists which have been penetrated by
porphyritic and syenitic rocks.

We do not pretend to have succeeded in unraveling the geolo-
gical structure of this most difficult and intricate region. There
are probably some powerful faults, whereby parts of the series are
repeated, while other portions are concealed from view; but we
could not satisfy ourselves as to the exact position of any one
dislocation. Besides faults, however, the district is greatly compli-
cated by the curvings and twistings of the beds, so carefully and
completely investigated by Playfair and Webb Seymour*, and by
Macculloch +.

We are unable to decide what relation the limestone of Loch Ran-
noch and Glen Erochie bears to that of Inverveck—the point where
limestone is first seen in descending the Garry. If we cculd suc-
ceed in identifying them, probably a great part of our difficulty
would be removed. The rock at Inverveck on the south-west side
of the Garry, 23 miles from Blair-Atholl, is a white, grey, or green-
ish crystalline rock, sometimes almost a steatite, with pale leek-
green, talcose lamine. ‘The strata are much broken, but the dip is
on the whole south-easterly.

In the grounds of the Duke of Atholl, especially along the
classic Glen Tilt, good sections are obtained of parts of this lime-
stone series, traversed by veins of granite and porphyry. There is
much local disturbance and great metamorphism at this locality.
Nowhere can this be better seen than in the deep wooded dell of
Glen Banavie, immediately behind Blair Castle. We first encounter
dark schists, greatly hardened and traversed by dykes of felspar-
porphyry, which have a N.N.E. strike. The strata have here no
determinate dip; indeed, the bedding is almost obliterated. Higher
up, however, the disturbance lessens ; and eventually the usual flag-
stones set in, with a steady south-easterly dip at 25° or 30°.

* Trans. Roy. Soc. Edinburgh, vol. vu. p. 303.

+ Trans. Geol. Soc. vol. ili. See especially Macculloch’s admirable descrip-
tion of Glen Tilt (oc. c7. p. 297). He speaks of granite having a foliated
structure, and of that structure being especially observable in the vicinity of
quartz-rock. He dwells particularly on the distinction between quartz-rock and
gneiss (p. 294), and shows that in Glen Tilt the general series consists of mica-
slate alternating in a yery irregular manner with hard argillaceous schist and

quartz-rock, and with a few beds of limestone (p. 291). The syenite and green-
stone of Playfair and Webb Seymour are called by him granite.

1861. ] MURCHISON AND GEIKIE—HIGHLANDS. 225

We ascended Glen Tilt as far as the Forest Lodge, where one of
us climbed the precipitous hill that forms the eastern side of the
glen. The whole of this region has been so minutely described by
the fathers of Scottish geology that we shall not venture to offer any
details, further than that the section of the east side of the glen,
opposite the Forest Lodge, shows very clearly that the limestone,
after sundry intercalations of schist, is overlain by a thick, massive,
white quartz-rock. This rock ought to be found in the Garry, but
we could not detect it, unless the hard thick-bedded grey quartz-
rock at Ault Clune, two miles below Blair, be its representative.

In the valley of the Garry at Blair and below it, there are pro-
bably at least two zones of limestone, one underlying the quartz-
rock, as does the limestone of Loch Rannoch, as well as that of
Glen Tilt, the other overlying the quartz-rock, like that of Loch
Kinardochy; but the whole of the sections in this part of the river
are very obscure*.

Blair to Dunkeld.—Passing over the obscured and doubtful ground
in the valley of the Garry below Blair-Atholl, we eventually meet
with quartzose and schistose strata, considerably contorted ; they are
seen here and there in the bed of the stream, particularly at the
bridge above the romantic Pass of Kilhecrankie. About three miles
and a half below Ault Clune, they change their dip from 8.E. to
N.W. ‘The series is then repeated; and at Pitlochrie the lime-
stone comes up again. From this point the latter rock strikes
across the hills in a north-easterly direction across Strath Ardle to
Glenshee, and thence into Glen Isla. How far it extends to the
south-west we did not ascertain. At the Pitlochrie quarry, the dip
is N. 10°.

The valley south of Pitlochrie, judging from the scanty sections
to be seen by the wayside, appears to run for two or three miles
upon the flagstones that underlie the limestone; two miles south
from that village a quarry has been opened in a micaceous quartzose
flagstone, which there dips N. 30° E. at 15°; and similar strata are
occasionally seen in the channels of the smaller streams that descend
intothe Tummel. These quartzose strata probably roll over again to
the south-east ; for we soon come upon the schists. But the valley
is much obscured by alluvium, especially after the junction of the
Tummel with the Tay; and the time at our disposal did not allow of
excursions on either side of the Strath, to settle the relative boun-
dary-lines.

At Dunkeld the upper schistose series is displayed in force. The
great quarries south of Birnam have been opened in grey slate, the
beds of which dip N. 70° W. at 65°, and are traversed by a cleavage
(much less perfect than that of Easdale), the planes of which are
inclined in the same direction at 55°.

* Since our observations were made, we have communicated with Prof. Hark-
ness, and have found that he has detected the upper limestone skirting the flanks
of the Ben-y-Gloe Mountains, not far above Blair. His observations on this
district will form part of the paper already alluded to. As shown in the text,
we also met with the upper limestone at the Spittal of Glenshee; but this is ata
considerable distance from the Garry valley.

226 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 6,

“The cuttings of the Dunkeld Railway have shown the junction of
these slates with the overlying Old Red conglomerates. The slates
are there considerably twisted, and their edges are covered by a con-
glomerate, which consists mainly of felspathic matter, the pebbles
being for the most part rounded and subangular pieces of various
amygdaloidal and porphyritic felstones. It was evident at a glance
that these pebbles of igneous rock were not derived from the Gram-
pians, since they differed lithologically in a marked degree from
the felspathic rocks of the crystalline region. Another fact readily
observable was the great scarcity, in places the entire absence, of
any fragments of the metamorphic rocks of the neighbouring moun-
tains, or even of the slates on which the beds of conglomerate rest.
The inference we formed was, that these conglomerates were derived
from volcanic ejections during part of the Lower Old Red Sand-
stone period; and this was speedily confirmed by finding, inter-
stratified with the conglomerate, a band of dark compact amygdaloidal
felstone, above which the conglomerate became exceedingly coarse,
and contained large detached masses of this same felstone. The
strata become finer as they recede from the junction with the slates,
and to the south pass gradually upwards into sandstones.

Spittal of Glenshee to Blairgowrie.—The last traverse which we
made this summer was from the Spittal of Glenshee, down that glen,
to Blairgowrie and Dunkeld. From the Spittal a glen called Glen
Beg branches off to Braemar in a N.N.E. direction. Its western
side is formed by a line of limestone which also ranges south-
east for nearly a mile. It resembles the limestone of Blair, and,
lke it, is interstratified with talcose, chloritic, and micaceous
schists. Some of these schists are carbonaceous, losing 15 per cent.
of their weight after ignition*, and present a remarkable wavy bed-
ding, with foliated surfaces, and a kind of rude cleavage. The
number of different bands of limestone is great in this locality, and
their changes of dip and strike endless. With a tolerably persistent
N.N.E. strike, they overlie the Ben-y-Gloe quartz-rock, and range
up Glen Beg, crossing the watershed, and descending again to
Braemar. Syenite and porphyry abound, in the form of large amor-
phous masses or dykes and veins.

On the east side of Glen Beg, the beds at the watershed have a
marked §.E. dip, which continues also in the quarry about a mile
nearer the Spittal. But much careful work is needed in this highly
altered region before its geological details can be thoroughly under-
stood. Limestone, with a northerly dip, has been quarried two
miles south of the Spittal, the intermediate ground being occupied
by gnarled schists.

Much felspathic rock (syenite or porphyry) occurs on both sides of
the glen. The strata become very quartzose, in gentle undulations, as
we proceed southwards ; and at Lair, a small cottage about two miles
from Dalrelzian, they are micaceous flagstones, dipping 8.E. at 8°.

* These schists will be referred to in a subsequent paper, in which we propose

to indicate the distinction between foliation and cleavage. The carbonaceous
schist was analysed by Mr. Tookey of the School of Mines.

1861.] MURCHISON AND GEIKIE—HIGHLANDS. 227

At Dalrelzian, limestone is again quarried. This band has a
westerly dip at the quarry; but its general range is from §.W. to
N.E., as it occurs in Strath Ardle, south of Kirkmichael, and crosses
by the southern flank of Mount Blair into Glen Isla. It is suc-
ceeded by gnarled schists, and these again at the Bridge of Cally
by slates, which have a decided S.E. dip at a high angle. In a short
distance, however, the slates take a north-west dip, as they do at
Birnam ; and at Rattray, a little north of Blairgowrie, they are
overlain by the conglomerate of the Old Red Sandstone.

Eastern Flanks of the Grampians.—It was a special object of one
of us in a former year to re-examine the schistose rocks on the
eastern flanks of the Grampians in Kincardineshire and Forfarshire.
This was done in two traverses on different parallels in 1827 and in
1859; and in both of these the succession was found to be similar.
In fact, a perfect conformity between argillaceous schists with some
limestone, and certain micaceous schists lying nearest to the interior
of the chain, was found to prevail. Numerous bosses of porphyry,
not laid down on any map, were also observed; and around these
granitic, syenitic, or other amorphous rocks, the highly broken strata
assumed a gneissic character.

Any one who is acquainted with those localities, 2. ¢. the valleys
of the Bervie Glen, west of Laurence Kirk, of the North Esk, the
Prosser, and South Esk, and will now read our descriptions of the
superior schistose and slaty rocks with limestone in the south of
Islay, cannot doubt that on the east flank of the Grampians we have
a repetition of the upper portion of the same great series, the dif-
ferent members of which we have traced in vast undulations from
N.W. to 8.E. In fact, the detailed and faithful description of the
transverse valley of the North Esk by Colonel Imrie, which was
read in the year 1804*, may be still referred to, after so long an
interval, as being in itself a full and copious illustration of our
upper series; though, when that paper was written, the author, as
well as most of his contemporaries, believed that all such Grampian
primary schistose strata had been accumulated at a period long an-
terior to the existence of life upon the surface of the globe.

In this section we also meet with the valuable proof that all the
so-called slates were in truth layers of subaqueous deposit, inasmuch
as they alternate over and over with what Colonel Imrie called
his “ aggregate rock,’ or, in other words, strata of broken mate-
rials accumulated in ancient seas. As this section was examined
on foot by one of us in company with Professor Sedgwick in 1827
and found to be quite correct, we now see how completely the facts
accord with all our subsequent observations on other flanks of the
Grampians.

Whilst on this occasion we are unprepared to enter into a detailed
description of the Grampians, we feel assured, from examination of
the flanks of these mountains on many points of the compass, that
the strata which there exist belong, on the whole, to the upper
members of the crystalline stratified rocks of the Highlands, with

* Trans, Roy. Soc. Edinburgh, vol. vi. p. 1.

228 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

here and there an emergence of the quartz-rocks and limestones,
and that the granites, syenites, porphyries, and other igneous rocks,
which occupy so large a portion of the chain, are necessarily of
comparatively young age. We have indeed completely satisfied
ourselves, by ascending to the heights of Braemar on the one side,
and by entering into the heart of the chain from Aberdeen to Bal-
moral on the other, that whilst there are no clear proofs of the
existence of any altered rocks of even the lowest Silurian age, there
are certainly not in these mountains any strata of the Cambrian date,
and still less any traces of the fundamental gneiss of the North-
western Highlands and Islands.

The old notion, therefore, that the Grampians contain the nucleus
of the most ancient rocks in Scotland, must now be abandoned.

Apprnpix. By Sir Ropericx I. Murcuison.—February 6, 1861.

A memoir by Professor Nicol having been read before the Geo-
logical Society on the 19th December last, in which the author
exhibited several sections illustrating the relations and succession
of the stratified crystalline rocks of Sutherland, which were
directly at variance with the sections of the same localities which
had been published by myself (and confirmed by the observations
of Professors Ramsay and Harkness), I then explained, vivé voce,
how I conceived that Professor Nicol had been misled by assigning
much too great an importance to what I considered to be local
and partial disturbances only. I argued that local interferences
of eruptive rock in nowise set aside the broad data I had for several
years been accumulating, which prove the existence of a funda-
mental gneiss, as distinguished by imfraposition, direction of the
strata, and mineral characters from all the crystalline schists which
overlie those quartz-rocks and limestones that rest upon such older
gneiss. Professor Nicol, on the contrary, adhering to the views of
the older Scottish geologists (as represented in former maps of Scot-
land, and his own), considers vast masses of the rocks which I
ranked as overlying, to be simply the older gneiss brought up to the
surface, and placed in apparently overlying positions by enormous
upeast-faults. As his memoir has been published in the Journal of
the Geological Society*, I am bound to place on record that I hold
distinctly to the general accuracy of those sections which I published ;
and, believing that the alterations in them proposed by Professor
Nicol are either erroneous or founded on deceptive local appearances,
I consider that all his reasoning as founded thereon must fall to the
ground.

I will here advert to those sections of Professor Nicol which are
most important.

First, let us examine the section from Loch Eriboll (p. 92, fig. 5),
which passes across the ridge to the east of Eriboll House ; since this
is the very traverse made by Professors Ramsay and Harkness, as
well as by myself. In that diagram the author exhibits much which

* February 1861, vol. xvii. No. 65, p. 85, &e.

1861. ] MURCHISON—-HIGHLANDS, 929

is not to be seen between Eriboll House and the summit of the ridge.
The section is compiled from some disturbed beds which he observed
in a ravine at a certain distance on the strike of the formations, and
he thus introduces, beneath the real and visible section, in which all
the strata of the escarpment of the ridge are seen to dip to the E.S.E.,
an ideal subterranean complication. In doing this he commingles
the existence of a great fault with a stupendous underground twist
of the fundamental gneiss, which rock is not seen nearer to this spot
than five or six miles, and which at that distance has a strike en-
tirely discordant to the quartz-rocks there lying upon it. Yet this
deep-seated granitic and hornblendic gneiss has, it is suggested, not
only changed its direction, and been thrown up conformably on the
quartz-rock and limestone with a south-easterly dip, but has also
been transformed into a micaceous and chloritic schist, wholly
unlike any portion of the old gneiss !

My conviction therefore remains unaltered, that, excepting local
and partial disturbances, and the irregular intrusion of igneous rocks,
the order above Eriboll House is absolutely that which has been
published by myself and witnessed by my associates*. It demon-
strates, in short, a true ascending order and transition from quartz-
rocks and limestone below, into superior micaceous and chloritic
schists (upper gneiss), as first indeed observed thirty-three years ago
by Professor Sedgwick and myself at this very spot.

Secondly, Professor Nicol has brought forward sections across
the strata at points where they are much broken and affected by
local intrusion of igneous rocks (notably figs. 3, 4, and 6, pp. 88,
89, 93), in order to show that the intrusive rocks occupy such a place
as to indicate a line of great dislocation along which the older gneiss
has been heaved up to the surface. But this view has been shown,
in former memoirs as well as in the present communication, to be
unfounded, inasmuch as similar igneous rocks (felspar-rocks, por-
phyries, and syenites) re-occur at various horizons in the series of
crystalline rocks, and do not invalidate the general ascending order,
or change the general conformity of the strata.

Thirdly, at Assynt (see fig. 8, p. 96), the ascending section
from the Loch, as given by Professor Nicol, is made to terminate
with a limestone above the quartz-rocks; it being held by him that
there is no quartz-rock above the limestone, except such as is brought
into that position from beneath by upcast-faults. Now, in my own
section of the same locality+, an upper quartz-rock is shown to lie
conformably upon, and to succeed regularly to, the limestone ; and
in confirmation of the accuracy of this fact, and of the clear proofs
of a passage upwards from that limestone into a superior quartz-rock,
I have not only the testimony of Professors Ramsay and Harkness,
as previously cited, but that of Mr. Geikie, who, unaccompanied by
me, visited the same spot last summer, and saw unmistakeably clear

* Tn fact, if Prof. Nicol’s section be viewed as respects the portion of the strata
which can alone be seen, it is almost identical with my own. (See Prof. Hark-
ness’s section, Quart. Journ. Geol. Soc. Aug. 1859, vol. xvi. p. 231, fig. 9.)

t Quart. Journ. Geol. Soc. Aug. 1859, vol, xvi. p. 217, fig. 3.

VOL, XVII,— PART I, BR

230 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 6,

evidence of the existence of an upper quartz-rock, under which the
limestone passed without any break *.

Fourthly, I simply repeat the statement I previously made, that
there are the most essential distinctions between the old and funda-
mental gneiss of Loch Stack and Loch More on which the quartz~
rock and limestone repose, and the earthy and slightly micaceous
flagstones which overlie such rocks on Loch More, and specimens of
which to compare with the older gneiss are exhibited. See Professor
Nicol’s section, fig. 6, and my section, vol. xvi. p. 226, fig. 6. Here
again the strike of the old or Laurentian gneiss (a) is nearly at right
angles to that of the overlying flag-like schists (d') with which
Professor Nicol unites it.

Fifthly, I am compelled to pomt out, in defending the correct-
ness of my own views as regards the relations of the rocks in Durness,
that the second of the sections of Professor Nicol (p. 87) is, on the
face of it, very inaccurate. The author gives this line of section as
proceeding from Far-out Head on the west to Kean-na-binn on the
east. Now the fact is, that this line is really from N. by W. to
S. by E. (see Map of Sutherland and Admiralty Charts). Owing to
this error, the strata are necessarily placed in false positions; for
those of the Far-out Head, and the promontories extending to the
Bishop’s Castle, and which dip away to the east, are, as I have shown,
the overlying thinly laminated schists with white sandy micaceous
flagstones 7, and are quite distinct, by position as well as structure,
from the nearest old granitic and hornblendic gneiss, which, striking
from N.N.W. to §.8.E., dips to the 8.8. W.

Si«thly, I would observe, that the section fig. 9, p. 100, from
Cnoe Chaorinie to Alt Ellag, as given by Professor Nicol, seems
essentially to sustain the proofs of the order of succession which I
have pointed out ; for in it we see a lower quartz-rock and limestone
followed conformably by overlying quartz-rocks and limestones,
whilst these are succeeded, also conformably, by chloritie schists.
The only difference between this section and my own view of the
succession in that tract is, that neither my companions nor myself +
could observe the fault or dislocation§ which Professor Nicol has

* See also Prof. Harkness’s sections in my memoir, Quart. Journ. Geol. Soe.
Aug. 1859, vol. xvi. p. 221, fig. 4, and p. 228, fig. 5.

t Specimens of these thin flag-like sandy schists from this promontory were
exhibited at the Meeting to show their entire dissimilarity to the old gneiss of
Kean-na-binn and the ridge S. of Durine Inn, with which Prof. Nicol connects
them.

t Professor Ramsay sedulously explored this locality by himself.

§ In a letter recently addressed to me by Professor Harkness, in which he
points out other errors in the sections of Professor Nicol, which I do not here
mention, he thus alludes to the introduction by Professor Nicol of the fault near
Alt Ellag between the quartz-rocks and the overlying chloritic, micaceous, and
gneissose rocks :—‘ Of this fault suffice it to say, that there is not the slightest
evidence of any crack here.”’ Tt has naturally given me great satisfaction to haye
the support of such an able and. independent observer as Professor Harkness,
who, when he visited the west of Sutherland, after a discussion which had taken
place on those very points at the Aberdeen meeting of the British Association,
had, as he himself writes, “a stronger feeling towards Nicol than yourself, so
that I may be said to have to some extent prejudged the case; when, however,

1861. ] MURCHISON-——-HIGHLANDS, 231°

placed between the quartz-rocks and limestones and the overlying
chloritic and somewhat gneissic schists.

In referring to the concluding pages of Professor Nicol’s last
memoir, I must remind him, that, when he calls for more proofs of
the continuance of the ascending order through the central and more
easterly parts of Sutherland and Ross than have as yet appeared, he
ignores what I have published on those very points. In 1858 I gave
a section from Loch Eriboll across the Moin to the Kyles of Tongue,
and in the following year I traced the ascending order with Professor
Ramsay from the inferior quartz-rock and limestone through oyer-
lying micaceous schist into gnecssic rocks, the latter being invariably
most prevalent when in the neighbourhood of eruptive masses of
granite and syenite. It was on that occasion that we first ascertained
that Ben Stomino (which in Professor Nicol’s map is represented as
Old Red Sandstone) was a granite. We had therefore already
answered Professor Nicol’s present query, and had shown that “the
huge syenitic domes of Ben Loaghal and Ben Stomino do not break
the series, and bring it under the lower and older gneiss*.” Again,
Professor Nicol writes as if Strath Oikel had not been examined,
though that tract was specially cited by myself as proving an as-
cending order; and when he says that no one has been in the
fastnesses of Fannich Forest, I may refer him to my own descrip-
tion of a great north-westerly fold of the overlying strata on Loch
Fannich +. In fact, if geologists will only take the trouble to read
my memoirs of 1858 and 1859, as published in the Journal of the
Geological Society, they will find many other proofs of the conti-
nuity of the ascending series to the eastern parts of Ross-shire,
and of their intense metamorphism and gneissic characters when in
contact with granitic rocks.

As Professor Nicol has endeavoured to show that my sections are
inaccurate, I may be permitted to point to the great discrepancy
between his earlier sections, published the year after he accompanied
me (his first visit to Sutherland), and those on which he now
relies. Denying as I do the accuracy of the last, I affirm that some
of his first or original sections are quite correct ; indeed they entirely
agree with my ownz. First, in the west of Sutherland, he shows,
as I have done, a fundamental gneiss (a), a red sandstone (6),
quartz-rocks and limestones, and a conformably overlying ‘upper
gneiss ” [sic] (f ) above the House of Eriboll. Yet now he has
composed the very different diagram for the same spot, and on that

I saw evidence so clear, I at once adopted your conclusions.” Professor Harkness
thus concludes his letter :—‘‘ The observations which I have since made, both in
other parts of the Scotch Highlands, and in the north of Ireland, haye still
further corroborated your conclusions; and, with reference to the hypothetical
views you expressed, I am convinced that the whole arrangement of rocks from
the fundamental gneiss to the upper gneissic rocks, &c., as recorded in your
memoirs, is the true sequence of the strata which make up the older sedimentary
series of the Highlands of Scotland.”
_ * See Prof. Nicol’s Memoir, Quart. Journ. Geol. Soc. vol. xvii. pp. 112, 113.

ft Quart. Journ. Geol. Soc. vol. xv. p. 387.

t See Quart. Journ, Geol. Soe. vol. xiii. pp. 22, 23.

R2

232 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

diagram I have already dilated. Next, in his old sections on Loch
Broom, his order of the quartz-rock and limestone, conformably
overlain by his ‘“‘ upper gneiss,” is equally clear, and is entirely in
unison with the section made by my companion last summer and
with my old observations. In short, his “ older gneiss” lying be-
neath all the other rocks is a, and his ‘‘ upper gneiss ” (6) is high in
the ascending series.

I say, therefore, in citing his own observations and sections, that
there is an “ upper gneiss ;”’ and to whatever “old, long-established
principles of Scottish geology” Professor Nicol may appeal, I main-
tain that the researches of my contemporaries and myself have neces-
sarily led to the establishment of the new classification.

In conclusion, I may say, that our labours during the last
summer, as detailed in the preceding memoir, seem to me to have
determined the question at issue, by an appeal to the order exhibited
over other and very extensive Highland regions. Thus, Mr. Geikie,
taking up the survey of the mainland, whilst I was exploring the
Laurentian gneiss of the Lewis, has followed the disputed line of
junction from Sutherland through mountainous tracts of Ross-shire
for more than sixty miles, and, by observing closely a number of
transverse sections, has completely established the proofs of a regular
and unbroken ascending order from the inferior quartz-rock and
limestone into overlying quartzose and micaceous strata (occasionally
assuming gneiss-like characters), which, graduating up into chloritic
schists and clay-slates, occupy such vast breadths of the north of
Scotland. On my own part, I have, during last summer’s survey
with my associate, so satisfied myself of the existence of the same
ascending order, not only in many parts of my native county of
Ross, but also by researches in the Southern Highlands, and notably
in Islay, as explained in the preceding memoir, that, bemg now
convinced that the principle of classification I suggested is esta-
blished on a sound basis, [ take my leave of the subject, trusting to
Mr. Geikie and my other able colleagues of the Geological Survey,
as well as to Professor Harkness and younger ecologists { than myself,
to discover new truths, which may improve or modify my con-
clusions.

On the Corxcrpencr between Srrariicatton and Forrarron in
the CrystaLttinE Rocks of the Scorrisa Hieutanps. By Sir
Roperick I. Murcuisoy, D.C.L., V.P.G.S., F.R.S., &c., and
ArcaIBatp Gerxir, Esq., F.R.S Es F.G.S.

{Read February 20, 1861, but, by permission, printed here in association with
the foregoing paper, which has reference to the same country. |

No memoir on the erystalline rocks of the Highlands of Scotland

can be regarded as complete if it contain no reference to the ques-

tion of the “foliation” in that region, as first raised in the year

1852 by the late Mr. D. Sharpe. In our paper which was laid

before the Society at the last Meeting, we avoided entering upon

this subject, reserving such remarks as we have to offer for a sepa-

1861.] MURCHISON AND GEIKIE—STRATA OF THE HIGHLANDS, 233

rate communication. At the same time we must specially refer to
our preceding memoirs on the structure of the Highland crystalline
stratified rocks, in which we have shown that the different mineral
formations which succeed to each other offer distinct proofs of
original deposit under water, some of them even containing organic
remains. Our conviction of the truth of this view has been arrived
at, not by any theoretical hypothesis, but by repeated and long-
continued observations of the succession and nature of the stratified
Highland rocks; and hence we are under the necessity of recording
our dissent from the opinions of a distinguished geologist now no
more, who, in a memoir published in the ‘ Philosophical Trans-
actions,’ and illustrated by a map and sections, has endeavoured to
prove that the very lines which we refer to deposit are lines of a
foliation which is the ultimate stage of the action of cleavage. We,
on the contrary, referring to our former memoirs for our proofs of
sedimentary deposit, will now point out that wherever cleavage
does exist in these Highland rocks it is transverse to those lamine
which have been referred to foliation by Mr. Sharpe, and which
we consider to be simply crystallized stratification.

In the early days of Scottish geology, it was shown by the illus-
trious Hutton and his contemporaries, that the gneiss and schists
of the Highlands were truly sedimentary formations, and that their
present crystalline structure arose from the action of heat at a
period posterior to their deposition. Subsequently the same views
were entertained and promulgated on all occasions by Macculloch,
during and after his numerous explorations of the Highlands.
Those eminent geologists and their successors, during many years,
never doubted that the planes or laminz of the schistose rocks
represented former lines of stratification, and they wrote of the dip
and “stretch” or strike of these altered rocks precisely as they
would have done had they been treating of unaltered sandstones,
shales, and limestones. But, after the publication, in 1846, of Mr.
Darwin’s observations on the metamorphic rocks of South America,
attention was drawn more pointedly to the structure and origin of this
class of rocks. That distinguished naturalist believed that, in the re-
gions of Chili and Tierra del Fuego, the planes along which the sepa-
ration of the crystalline particles had proceeded did not coincide with
the original planes of bedding, but with the planes of cleavage. He
‘proposed to apply the term “foliation” to the laminar arrangement
of gneiss and schist—a term to which, if used merely to express
this arrangement, without reference to its origin, we haye no objec-
tion. But Mr. Darwin considered that his observations bore out
the general inference, that foliation and cleavage are parts of the
same process,—‘‘in cleavage, there being only an incipient sepa-
ration of the constituent minerals ; in foliation, a much more com-
plete separation and crystallization* :” and he applied this theory
to the elucidation of large tracts of South America.

Now, however this doctrine may be borne out in regions which
we have not seen, we hold that it is utterly inapplicable to the

* Darwin, Geol. Obs. South America, pp. 106-160.

234 PROCEEDINGS OF THE GHOLOGICAL SOCIETY. [Feb. 20,

Highlands of Scotland, or to any mountain-tracts in Europe which
we have explored. In fact, all our contemporaries, with whom or
with whose works we are acquainted, have treated such laminz
as marking, on the whole, the lines of original stratification. Thus,
in 1827, when one of us explored the Highlands with Professor
Sedgwick, that distinguished man clearly pointed out, i situ, the
absolute independence of such foliation and cleavage ; and thence-
forward, and after repeated surveys of the same region during suc-
cessive years, we have, on various occasions *, expressed our entire
dissent from the doctrine and opinions of the lamented Mr. Daniel
Sharpe, recorded in a memoir entitled “On the Arrangement of
the Foliation and Cleavage of the Rocks of the North of Scotlandt.”
As early indeed as the year 1835, and consequently eleven years
before Mr. Darwin wrote, and seventeen years before the publica-
tion of Mr. Sharpe, Professor Sedgwick, in his remarkable “‘ Me-
moir on the Structure of large Mineral Masses,” actually enunciated
the distinctions on which we insist in this memoir. In speaking
of those crystalline schists of parts of England and Wales, and of
the Highlands of Scotland, which are “ finely foliated,” he goes on
to say :—‘ In general, however, the foliated uneven layers of these
older formations belong, I believe, to beds, and not to cleavage-
planes; and the oldest and most crystalline rocks, designated by
the general term of schists, have no true slaty cleavage in the sense
in which I have used the term 7.”

Professor Sedgwick thus defines these distinctions :—‘“ Bed is
always applied as the English synonym of stratwm; and the words
thick-bedded, thin-bedded, thick-flaggy, thin-flaggy, and laminated,
are words in common use, and express well enough different modi-
fications of stratified structure. ‘The term foliated, again, expresses
very well the peculiar structure of mica-schist, and the fine, glossy,
undulating layers of greywacke.” After enumerating the essential
difference between slaty and flaggy structure, he adds :—“ In this
way, foliated as distinct from laminated, and slaty as distinct from
Slaggy, become terms of a definite meaning §.”’

It should be further remembered, that in the year 1840, and also
before Mr. Darwin’s observations were published, the Local Di-
rector of the Geological Survey, Professor Ramsay, devoted himself
specially to a careful survey of Arran, and in the early part of the
following year published a descriptive account of the geology of
that island. In speculating upon the origin of the quartz-layers
that are interbedded in its schists, he remarks that these quartz-
layers “lie in regular laminee, very numerous, and parallel to the
plane of stratification. Sometimes these alternations are almost
as minute as the leaves of a closed volume.” He thus clearly

* Report Brit. Assoc, Glasgow, 1855, Trans. of Sections, p. 86. Siluria, 2nd
edit. pp. 179, 195. Quart. Journ. Geol. Soc. vol. vii. p. 168 ; and vol. xv. p. 391.

t See Philosophical Transactions, vol. exlii. p. 445 (1852); with a coloured
map of Scotland and sections.

{ Trans. Geol. Soc., new series, vol. ili. p. 479. 7

§ Ibid. p. 480.

1861.] MURCHISON AND GEIKIE—STRATA OF THE HIGHLANDS. 235

recognizes the existence of stratification-planes, and the parallelism
of these as a whole with the interlaminations of quartz *.

The late Mr. Daniel Sharpe, in his memoir, endeavoured to prove
that the foliation-lamine of the gneiss were arranged in great arches,
ranging ina N.K.and§8.W. direction. But true slaty cleavage, as we
have already remarked in our preceding memoir, is rarely met with
in the Highlands, and where it does occur, it is nearly always
more or less transverse to the planes of stratification. Again, whilst
Mr. Sharpe does adyert to rare examples of cleavage-planes tra-
versing those lamin which he refers to foliation (Phil. Trans. 1852,
vol. exlii. p. 449, and pl. 23, figs. 1, 3, 4), he maintains throughout
his memoir, and illustrates the view in his general sections, that all
those bands of different mineral matter which we have shown in
preceding memoirs to be successive deposits, are due to foliation only.
He altogether loses sight of the great intercalations of limestone, some
of which, as we have formerly shown, contain organic remains. Let
us now give some illustrations of our views.

At Dunkeld in Perthshire, at Hasdale in Argyllshire, or at Bally-
hulish, where true cleavage exists, it is seen to cut through those
lines of colour, by which, in finely levigated clay-slates of a homo-
geneous composition, the original laminz of deposit are recognized.
In the argillaceous schists on the flanks of the Grampians, and
notably near the Spittal of Glenshee, where the strata are often
violently contorted, as seen in the specimen we now exhibitt, the
cleavage-planes are rudely parallel to each other, and cut right
across the undulating layers of black carbonaceous schist, This
specimen is indeed a good example of the view now adopted, that
the parallel planes of cleavage are due to lateral pressure; for here
we haye a proof that the original beds of carbonaceous shale have
been so intensely squeezed up as to produce the contortions exhi-
bited, whilst the cleavage-planes traverse them. We have also at
hand in this locality the explanation of these contortions in the exist-
ence of numerous points or bosses of syenite, porphyry, and other
similar rocks, which protrude to the surface around the Spittal of
Glenshee. ‘The compressed schist to which we allude is so highly
carbonaceous in the little burn to the west of the inn at the Spittal,

* Professor Ramsay, in a paper read before the Geological Society (Quart.
Journ. Geol. Soe. vol. ix. p. 172), discusses the metamorphism of Anglesea, and
refers it to a period anterior to that of the cleavage of the Welsh slates. He
adds, that ‘“ if the rocks be uncleaved when metamorphism takes place, the folia-
tion-planes will be apt to coineide with those of bedding; but if intense cleavage
has occurred, then we may expect that the planes of foliation will lie in the planes
of cleavage.” And in the letter-press explanation of Sheet 40 of the Horizontal
Sections of the Geological Survey, he unhesitatingly declares his belief, that the
metamorphic rocks of Anglesea are the prolongation of the green and purple
grits and slaty rocks of Bangor ; and that, moreover, they are disposed along an
anticlinal axis, the 8.H. side of which consists of the higher part of the Cambrian
series, overlaid by the Lower Silurian, while the N.W. side brings down the
same succession, though broken by a line of fault, “ thus completing the series,
and adding to the probability of the Cambrian age of most of the metamorphic
rocks of Anglesea.”

+ This specimen is deposited in the Museum of Practical Geology.

236. PROCEEDINGS OF THE GEOLOGICAL society. [| Feb. 2

that some of the points of rock blacken paper like a black-lead
pencil, and we therefore supposed it might be graphite; but a che-
mical examination of it at the Government School of Mines by Mr.
C. Tookey has shown that it 1s simply highly carbonaceous black
schist, with some. mica, the rock yielding on combustion nearly 16
per cent. of carbon.

In arriving at the belief which we entertain, that all the “ foli-
ation’? of the crystalline rocks of the Highlands which we have
examined is nothing more than the original laminee of deposit under
water, of sand, clay, lime, mica, &c., which have been so altered as
often to segregate in one layer more mica, and more sand or clay
in the others, thus evolving felspathic, quartzose, and micaceous
crystalline laminee, we are sustained in our inference by an appeal
to the whole succession of the mineral deposits of the north of
Scotland. For we have shown that these successive deposits are so
knit together by transition and conformable superposition, that it is
quite impossible to exclude from the series those of its members
which still exhibit not only a mechanical origin, but also contain
organic remains. [rom our old acquaintance with the late Mr. D.
Sharpe, we are convinced, that if, instead of making one rapid survey
only, in which, full of a new theory, he naturally apphed it, with
his well-known energy, he had year after year examined these
Highland rocks, he would haye seen the impossibility of excluding
(as he did) the greater part of the quartz-rock of Scotland from
the crystalline series, merely, as he says, because it is “‘ an altered
sandstone of which the mineral character has been changed by plu-
tonic action.”” He would, we doubt not, on a more careful survey,
have seen that this very rock and its associated limestones are in-
tegral and even lower parts of a large portion of that same crystalline
series ; andthen he would have admitted, that, as these pure quartz-
rocks (evidently nothing but altered sandstones, and in which Anne-
lides and an Orthoceratite have been found) graduate into micaceous
quartz-rocks, mica-schists, and gneissose rocks, they could not be
divided geologically into two separate classes, but form truly one
great series, varying in its mineralogical characters as well as in the
extent and form of its metamorphism.

The views which we entertain have been indeed, to a great extent,
sanctioned by the examination of the older rocks of the Highland
border by a very close and accurate observer of structure. Di-
stinctly objecting to the general application of the term folration, Mr.
Sorby has shown that one of the structures of metamorphic rocks
‘has every character that would be the result of stratification, even
in some cases including the current structures *.”’

Again, the same author, in his notice of the microscopical nature
of mica-schist, has demonstrated, that in one class of these rocks the
flakes of mica lie in the plane of the alternating layers of different
mineral composition, whilst in the other class the flakes of mica
traverse the original lines of bedding like slaty cleavage. He there-
fore proposes the terms “ stratification-foliation ” and “ cleayage-

* Report Brit. Assoc. Ady, of Science, 1855, Trans. of Sections, p. 96.

~-

1861.] MURCHISON AND GEIKIE—-STRATA OF THE HIGHLANDS. 237

foliation.” The latter structure is partially to be seen in the schistose
rocks on the coast to the south of Aberdeen, which are highly meta-
morphosed, and have never been examined by us; but we have to
thank Mr. Sorby for the pertinent induction respecting them, ‘“ that
the peculiarities in the rocks having ‘ cleavage-foliation ’ cannot be
explained except by supposing that they have been metamorphosed
stratified rocks,” adding “ that the cleavage-foliation is the effect of
previously existing cleavage, and not that slaty cleavage is a partially
developed foliation*.”

In dissenting from the views of Mr. Sharpe on this one essential
point, we must add, that there are many passages in his memoir
with which we entirely coincide. Thus, nothing is more true than
his declaration, that the geographical separation between gneiss and
mica-schist and chloritic schist throughout the north of Scotland, as
laid down by Macculloch, has been drawn too arbitrarily. We fully
admit, and have shown, that many of the strata so defined by that
author have “ the same geological relations.” But when Mr. Sharpe
applied to their internal divisions the term “foliation,” and, separating
it entirely from stratification, contended that such foliation is the
ultimate term of the same action which produced slaty cleavage, we
are completely at issue with him.

Whether we admit, with Phillipst, Sharpet, Sorby§, Tyndall ||,
and others, that the parallel cleavage of rocks was produced by
mechanical lateral pressure of the strata, or, following the original
speculation of Sedgwick, conceive that it was the result of crystalline
and polar forces, it is quite obvious throughout the Highlands of
Scotland, that this action was not the same as the modus operandi,
whatever it was, which changed the original layers of sand, mud,
and lime into crystalline lamine.

In short, as the one set of planes traverses the other, and as the
straight lines of parallel slaty cleavage (wherever they occur) are
strikingly distinguished from the convoluted and twisted layers of
different colour and composition, we are at a loss to imagine how
these two results could ever have been referred to different degrees
of intensity of one and the same cause.

As we have already dilated on the true cleavage as affecting the
slaty rocks of Islay, Easdale, and the adjacent tracts of Argyll and
Ballyhulish, &c., it will be remembered that in rare instances only
does this feature coincide with the layers of deposit, any more than
in Wales and other slaty tracts. Even along the Highland border,
where Mr. Sharpe says that the foliation of the mica-schist and the
cleavage of the slate ‘are both vertical along lines so closely corre-
sponding that they may be considered continuous,” we found in
the slate-quarries of Dunkeld that there was a clear and manifest

* Report Brit. Assoc. Adv. of Science, 1856, Trans. of Sections, p. 78.

+ See Report Brit. Assoc. Ady. of Science, 1843, Trans. Sect. p. 60; and 1857,
p. 386, &e. ‘

t Quart. Journ. Geol. Soc. vol. iii. p. 74; vol. v. p. 111.

§ Edinb. New Phil. Journ. 1853, vol. lv. p. 187; Phil. Mag. 1856, xii. p. 127.

| Notices Royal Institution, June 6, 1856. —_—-

238 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

distinction between the planes of cleavage and the lines of deposit*
as marked by the colour of the slates. But the parallelism of the
mica-schist (a sandy quartzose micaceous rock) to the clay-slate
which succeeds, and to which Mr. Sharpe applies his remarks, is
indeed one of the phenomena on which we have been all along in-
sisting,—viz. that these different mineral masses of the Highlands
succeed to each other regularly, and are fairly linked together, so as
to form one great series.

In truth, if the observer follows any one mineral stratified mass
upon the strike of the beds, he will often find that what at one ex-
tremity of it was highly crystalline is at the other much more earthy
and unaltered. Again, if he examines many of the quartzose, schistose,
and calcareous masses, he cannot fail to observe the essential cha-
racters of ordinary stratified sediments, such as way-boards dividing
different mineral substances, wavy surfaces, joints, and all the con-
comitant appearances, including occasional gritty and even pebbly
layers.

In Mr. Sharpe’s map? there is one dominant feature which agrees
with our observations. He gives to the gneiss of the Lewis and
the western coasts of Sutherland and Ross a true north-westerly
and south-easterly strike, and thus exhibits it at right angles to the
strike of nearly all the other crystalline rocks of the mainland. But,
never having observed the true order of superposition of the different
mineral masses in the north-west, which is the foundation of all our
induction, he follows Macculloch and unites all these crystalline rocks
in one gneissose and micaceous series, and treats all our lines of
stratification (and as such they were viewed by Hutton and also by
Macculloch) as lines of “ foliation.” In fact, these so-called lines of
foliation, and the transverse sections of them which Mr. Sharpe exhi-
bits, may serve in a broad sense to represent our lines of stratification.
In his generalized and theoretical diagrams also, his arches corre-
spond in a general way with the lines of anticlinal axes; with this
difference. however, that he does not insert, as the complement of
anticlines, lines of synclinal troughs+, which, as we have shown in the
previous memoir, do really exist. He has, moreover, omitted alto-
gether the bands of limestone, which are of such importance in demon-
strating the coincidence of stratification-planes and lines of foliation,
and in working out the geological structure of the Scottish Highlands,

No better illustration, indeed, of our own views can be given than
by referring to Mr. Sharpe’s own sections. First let us take his
general sections, figs. 1 and 2, which in a traverse of ninety miles
across Scotland exhibit at least five great anticlinals, and all his lines
of foliation would be our lines of deposit. Next, in fig. 3, the mica~
schist of Ben Lomond (chloritic schist, by the by, in great part) is
represented as a “foliated” rock dipping to the 8.8.E., whilst we

* Mr. Sharpe's sections indeed prove this ; for the lines of cleavage in his fig. 1
traverse the lines of foliation, which latter are, according to our views, indications
of the layers of deposition.

+ Phil. Trans. 1852, plate 24.

¢ Unless his “fan-shaped” foliation represents the synclinals. -

1861.] MURCIHSON AND GEIKIE—STRATA OF THE HIGHLANDS. 239

affirm that it is most clearly a depositary rock, the lines of original
bedding of which coincide with the lines of metamorphism, since,
besides the alternation of variously coloured schistose layers, there
is really an intercalated bed of white quartzose and rounded pebbles,
thus clearly proving the whole to have been originally a mechanically
formed deposit. And, again, this one section in itself demonstrates
the utter disconnexion between such true stratification-planes and
cleavage ; for in advancing to the 8.E. into the overlying deposit of
clay-slate, its layers (folia of Sharpe) are found to be traversed by a
real slaty cleavage of which there is not a trace in Ben Lomond.

In fig. 4, where the section crosses Loch Tay, and where the dark
schists have no cleavage, Mr. Sharpe omits the great feature of the
case, the presence of those regularly bedded limestones which dip
under Ben Lawers: and, if he had taken time to examine the internal
structure of the country further to the N.W., he would have found
other limestones reappearing together with the inferior quartz-rock
beyond Glen Lyon, in the Loch and Moor of Rannoch, thus forming
the other side of a great trough.

His section across Glen Shee (fig. 5) is another indication of those
undulations of the upper schistose strata which we have observed.
In that tract we have already demonstrated that the contortions of
the original strata of black carbonaceous schist are traversed by lines
of parallel slaty cleavage*, thus showing even in a hand-specimen
the complete independence of cleavage from those lines in the cry-
stalline rocks which are true lines of bedding and are wholly uncon-
nected with slaty cleavage.

When Mr. Sharpe affirms that the contortions of gneiss and mica=
schist ‘‘ are far more complex than are ever found in the most dis-
turbed strata, and are such as could only be produced in matter in
at least a state of semi-fluidity,” we refer the reader to the intensely
curved Carboniferous strata in Bride Bay, Devonshire, or to the num-
berless contortions of the Devonian rocks of the Rhine. In the
Silurian schists of the Lammermuir Hills, and numberless “ grau-
wacke”’ rocks in other tracts, both abroad and at home, multitudes
of similar rapid foliations have also been effected after the strata had
been accumulated, and probably before they underwent that change
by which they have passed into a highly crystalline state.

Again, in tracing the folds of the differeat mineral masses through
the north of Scotland and in laying them down on maps, we have
convinced ourselves that the strata so reappear on various parallels
and so exhibit repetitions of the same geological relations to each
other, 2. ¢. the quartz-rock and limestone occupying one zone, and
the mica-schists, the quasi-gneiss, and clay-slates another, that the
effort made by Mr. Sharpe to unite them in one crystalline mass,
which had been thrown into arches through the process of “ foliation,”
is, We conceive, antagonistic to the true principles of geological in-
ductive reasoning.

Looking at these different mineral masses, whether as they succeed
to each other, or as they often gradually change their lithological

* Indicated also in Mr. Sharpe’s fig. 5.

240 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20.

character in their lateral extension, as well as in their succession
from quartz-rocks into mica-slates and vice versd, and seeing that in
some of their members they contain Silurian fossils, we have natu-
rally come to the conclusion, that on the whole the crystalline strati-
fied rocks of the Highlands are simply the metamorphosed equivalents
of the Silurian grauwacke of the Southern Scottish counties, in which
there is quite a large enough area of varied mineral matter to account
for the greater part of such stratified crystalline rocks, particularly
when we reflect on the enormous masses of granite, porphyry, and
syenite which prevail in the North.

In conclusion, we express our belief that the so-called “ foliation ”
of the Highland rocks is, on the whole, nothing more than such an
alteration of the original deposits as caused the siliceous, felspathic,
and micaceous ingredients to form separate layers, as seen in some
instances, though in others they are intermixed in the same layer,
and in some parts are simply altered sandstones and limestones with
organic remains. In certain cases, like those pointed out by Mr. Sorby,
there may doubtless be cleavage-foliations in the mica-schist, but
these are clearly exceptions to the general rule.

Although we cannot here enter upon the great problem of how
such changes in the character of the strata have been brought about,
yet, looking to those researches in this line which have already been
made (by M. Bischoff, M. Daubrée, M. Delesse, M. Deville, Mr. Sterry
Hunt, and others), we confidently anticipate that the experiments of
the chemical geologist will ere long solve the mystery, and in doing
so we trust that they will confirm the conclusions at which we have
arrived by a survey of the phenomena in the field.

241

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From November 1st to December 31st, 1860.

I, TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. Vol. xxx.
No. 90. November 1860. From Prof. Silliman, For.M.G.S.

E. Billing’s ‘Additional Note on the Potsdam Fossils,’ 337.
L. Lesquereux.—Coal-formations of North America, 367.
C. Lea.—Numerical relations between Equivalents, 399,

L, Playfair.—Numerical relations between the Densities and Equi-
yalents of certain Elements, 420,

Art-Union of London, Report for 1860.
Assurance Magazine. Nos. 40, 41.
Atheneum Journal for July—October 1860. Nos. 1706-1722.

Notices of Scientific Meetings, Xe.

Meeting of the British Association, 18, 59.

Meeting of the International Statistical Congress, 94, 128.

A. Gray.—The Origin of Species, 161. i

J. W. Dawson’s ‘ Archaia,’ noticed, 198.

G. Buist and J. E. Tennent.—Fresh water in Coral Islands, 196, 229.

H. James, J. B. Jukes, G. B. Airy, W. E. Hickson, and H. Hen-
nessy.—Change of Climate, 256, 325, 355, 384, 385, 416, 450, 483,
515.

J. Tyndall’s ‘The Glaciers of the Alps,’ 280.

A. K. Johnston.—Ben Nevis, 325.

R. Damon’s ‘Handbook to the Geology of Weymouth,’ noticed,
370.

J, R. Leifchild’s ‘Sketch of the Geology of the Counties of Glou-
cester and Hereford,’ noticed, 375.

J. Rogers.—Earthquake in Kent, 357, 387.

©. Daubeny’s ‘ Remarks on the Origin of Species,’ &c., noticed, 887.

J. D. Forbes’s ‘Reply to Professor Tyndall’s Remarks,’ &c., 422.

J. 5. Henslow.—Flints in the Drift, 516.

242 DONATIONS.

Atheneum Journal for November and December. Nos. 1723-1731.

Meetings of Scientific Societies.

C. R. Bree’s ‘Species not transmutable, nor the Result of Secondary
Causes,’ noticed, 585.

J. §. Henslow.—Flint-hatchets in the Drift, 592.

F. L. M‘Clintock.—North Sea Soundings, 670.

G. B. Airy.—Change of Climate, 670.

W. EK. Hickson.—Changes of Climate, 831.

G. C. Wallich’s ‘ Notes on Animal Life in deep sea,’ noticed, 833.

J. Phillips’s ‘ Life on the Earth,’ noticed, 907.

W. B. Clarke’s ‘Researches in the Southern Gold- fields of New
South Wales,’ 9153.

Basel, Verhandlungen der Naturforschenden Gesellschaft in. Zweiter
Theil. Viertes Heft. 1860.

C. F. Schoenbein.—Chemische Notizen, 419-520,

Berlin. Abhandlungen der Konig, Akad, der Wissensch. Aus dem
Jahre 1859. 1860.

——. Preisfrage d. phys.-math. Klasse d. K. Preuss. Akad. d. Wiss.
fiir das Jahr 1863.

Zeitschrift der Deutsch. geol. Gesellschaft. Band xii.
Hett 1. November 1859-January 1860.

Verhandlungen der Gesellschaft, 1-12.

Briefliche Mittheilung gen, 13.

C. Lossen.—Ueber einige Lituiten, 15 (plate).

G. vom Rath.—Skizzen aus dem vulkanischen Gebiete des Nieder-
rhein, 29.

— Hosius.—Beitriige zur Geognosie Westphalens, 48 (map).

K. y. Fritsch. —Geognostische Skizze der Umger end yon Ilmenau
am Thiringer Walde, 97 (map and 2 plates).

J. G. Bornemann.—Ueher einige Foraminiferen aus den Tertiarbil-
dungen der Umgegend yon Magdeburg, 156 (plate).

O. Griepenkerl. —Eine neue Ceratiten-Form aus dem untersten
Wellenkalke, 160 (plate).

Bombay Geographical Society. Transactions. Vol. xv. 1860.

G. Buist.—Geology of Lower Egypt, 1.
A. W, Stiffe—Hot Springs of Bosher , near Muscat, 123 (map). .

Calcutta. Journal of the Asiatic Society of Bengal. New Series.
No, 104. 1860, No. 3.

J. Obbard.—Translation of waves of water with relation to the
Flood of the Indus in 1858, 266.

J. H. Pratt.—Waves of Translation and River-flood of the Indus,
274.

Canadian Journal. New Series. No. 30. November 1860.

C. Robb.—Physical Geology of Western Canada, 497.

E. J. Chapman.—Minerals “and Geology of Canada, 517.

R. Owen’s ‘ Paleontology,’ noticed, 538,

C. F. Rammelsberg’s ‘Handbuch der Mineralchemie,’ noticed, 540,
J. Hall—Formation of Mountain-ranges, 542,

DONATIONS, 243

Canadian Journal (continued).
E. J. Chapman.—Rules for calculating the thickness of inclined
Strata, 544,
Canadian Expeditions to the North-west Territory, 545.

Canadian Naturalist and Geologist. Vol. v. No.5. October 1860.

Life of David Douglas [ Volcanos of Hawaii], 329,

Acton Copper-mines, 349

J. W. Dawson.—Earthquake of October 1860, 363.

Lord Wrottesley.—Address to the British Association, 382.

Critic. Vol. xxi. Nos. 539-547,
Meetings of Scientific Societies, &e.
J. Phillips’s ‘ Life on the Earth,’ noticed, 671.

C. S. Forbes’s ‘Iceland, its Volcanos, Geysers, and Glaciers,’ noticed,
806.

Dublin Geological Society. Journal. Vol. viii, Part 3, 1860.

H. T. Geoghegan and B. T. Patterson.—Section through the Silurian
and Carboniferous Strata of Hook Head, Wexford, 187.

8. Haughton.—Geology of the Arctic Archipelago, 196.

G. H. Kinahan.—A Reversed Fault in the Leinster Coal-field, 213.

Anniversary Address, 227.

W. H. Baily.—Corynepteris, a new fossil Fern and other fossil
plants from Limerick, 237 (plate).

R. H. Scott—A new metallic ore from the Connorree Mines,
Wicklow, 241.

A. Gages.—Formation of Orpiment in a mass of Sulphate of Barytes,.
from the Carboniferous Limestone of Tipperary, 243.

ae, B. Wynne.—Mining-districts of Silvermines, Tipperary, 244
map).

J. Kelly.—Greywacke rocks of Ireland and England, 251.
——. Journal of the Royal Dublin Society. No.1. April 1856.

No. 11. October 1858.
EK. Byrne.—Separation of Copper and Iron by Ammonia, 146,

—_——
.

Geneva. Société de Géographie de Généve. Mémoires et Bulletin.

Vol.i. Part 1. Juin 1860. From Sir C. Lyell, V.P.GS.
F. Berton et Degroot.—Découvertes métallurgiques dans Californie,
23 (map).

Geologist. Vol. iii. Nos. 35, 36. Nov. and Dec. 1860.

S. J. Mackie.—Geology of Folkestone, 393.

A. Delesse.—Pseudomorphs, 396. one

5. J. Mackie.—Fossil Flint Implements, 404.

G. E. Roberts.—Geology of the Severn Valley Railway, 433,

C. Moore.—New Jurassic Brachiopoda, 438 (plate).

T. Austin.—Protoechinus anceps from Hook Point, and Palechinus,
446 (figure).

T, R. Jones.—Wealden Paludine and Uniones, 448 (plate).

Proceedings of Societies, 408, 454.

Notes and Queries, 416, 458,

Reviews, 423, 464,

244 DONATIONS.

Geologists’ Association. Proceedings. No.5. 1860.

C. Tomlinson.—The action of heat on certain Sandstones of York-
shire, 50.

S. J. Mackie.—Flint Implements found in the Drift, 55.

W. H. Bensted.—The Kentish Ragstone as exhibited in the Igua-
nodon-quarry at Maidstone, 57 (plate).

C. B. Rose.—The Mastoid appearance on some faced flints used in
buildings, 60,

Glasgow Geological Society. Transactions. No.1. 1860.
J. Young.—Geology of the Campsie District, 5 (2 plates).

Gratz. Fiimfter Bericht des geognostisch-montanistischen Vereines
fiir Steiermark. 1856. From Prof. Morris, F.G.S.

Hauptausweis iiber die im Herzogthume Steiermark gewonnenen
Bergwerks-Producte und deren Berwerthung: fiir das Militar-
Jahr 1854, &e.

F. Rolle.-—Ueber die im Sommer 1855 ausgefiihrten geognostischen
Untersuchungen im westlichen Theile yon Mittel- und Unter-
steiermark, 29.

A. Miiller.—Ueber die geognostische Erforschung der Umgebung von
St. Michael und Kvaubath in Obersteier, 53 (plate).

F. Seeland.—Ueber die geogn. Begehung der siidéstlichen Umge-
bung yon Leoben, 77.

——. Sechster Bericht. 1857.
Hauptausweise iiber die Bergwerks-Producte, &c., fiir das Jahr
1855.
F. Rolle-—Geogn. Untersuchungen im westlichen Theile yon Unter-
steiermark, 9.

-~——. Achter Bericht. 1859.

Th. y. Zollikofer.—Ueber die Ergebnisse der im Sommer 1858 in
Untersteier ausgefiihrten geognostischen Begehungen, 1 (2 pls.).
Hauptausweis tiber die Bergwerks-Producte fur das Jahr 1857.

Great Britain, Geological Survey of. Memoirs. 1860. From the
Director-General of the Geological Survey.

E. Hull,—The Geology of the country around Wigan.

—. Memos. 1860.
W. T. Aveline and R. Trench.—The Geology of part of Northamp-
tonshire (Description of Quarter-sheet No. 53 S.E.).
G. P. Wall and J. G. Sawkins.—Report on the Geology of Trinidad ;
or Part I. of the West Indian Survey.

——. Mining Records, 1860.

R. Hunt.—Mineral Statistics of the United Kingdom, &c., being
Part 2 for 1858.

BONATIONS. 245

Hobart Town. Papers and Proceedings of the Royal Society of Tas-
mania. Vol. ii. Part 2. 1859,

C. T. Downing.—Norfolk Island, 195.
Horticultural Society. Proceedings. Vol.i. Nos. 18, 19.

Institution of Civil Engineers, Proceedings. Vol. xvii. Session
1858-59. 1859.

M. B. Jackson.— Water-supply to the City of Melbourne, 563.

Institut, ?. Sect. I. Nos. 1896-1406. Seet. If. Nos. 294, 295
(in one).

Meetings of Scientific Societies, &c.
Linnean Society. Journal of the Proceedings. Vol. v. No. 18.
Literary Gazette. New Series. Vol. v. Nos. 124-131.

Meetings of Scientific Societies, &c.

G. Grote’s ‘ Plato’s Doctrine respecting the Rotation of the Karth;
and Aristotle’s comment upen the Doctrine,’ noticed, 411.

C. R. Bree’s ‘Species not transmutable,’ noticed, 450.

J. Phillips’s ‘ Life on the Earth,’ noticed, 490.

Liverpool. Transactions of the Historic Society of Lancashire and
Cheshire. Vol. xu. Session 1859-60. 1860.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xx. Nos. 134,135, & 136 Suppl. Nov. and Dec. 1860. From
Dr. W. Francis, F.G.S.

R. Schneider.—Volumetric determination of Antimony, 342.

A. and F. Dupré.—Spectrum-analysis of London Waters, 373.
Scheibler.—The Tungstates, 374.

Wohler.—New Salts of Suboxide of Silver, 376; Titanium, 377.
Caron.—Metallie Calcium, 376.

Michel and Wohler.—Alloys of Aluminium, 377.

Heintz and Richter.—Artiticial Boracite, 378.

Nordenskjold and Chydenius.—Crystallization of Thoria, 378.
E. Lartet.—Arrow-heads in a cavern in Languedoc, 400.

T. F. Jamieson.—Crag-shells in Aberdeenshire, 401.

R. Owen.—Fossil Vertebrze from Frome, 401.

B. Wood.—Fusible Metal, 403.

R. A. Smith.—Arsenic in Coal, 408.

D. Forbes.—Darwinite, a new mineral from Chile, 425.

O. Fisher.—Denudation of soft Strata, 483.

J. W. Dawson.—Fossil Fern from Nova Scotia, 485.

C. Rickman.—Section and Fossils at Dulwich and Peckham, 486.

Longman’s Notes on Books. Vol. ii. No. 23. Nov. 30, 1860.
Mechanics’ Magazine. New Series. Vol. iv. Nos. 97-103, 105.

Meetings of Scientific Societies, &c.
VOL. XVII.—PART I. 8

246 DONATIONS.

Moscow. Bulletin de la Soc. Imp. des Naturalistes de Moscou.
Année 1859. No.2. 1859.

H. Trautschold.—Ueber Petrefakten vom Aralsee, 303 (3 plates).

I. Njenkof.—Analyse des Honigsteins, aus der Kohlengrube von Ma-
lavka im Gouvernment Tula, 547.

G. Kade.—Ueber Lituus perfectus, Wahlenb., 621.

——, ——, Nos.3sand4. 1859.

H. Trautschold.—Recherches géologiques aux environs de Moscou,
109 (2 plates).

R. Hermann.—Ueber die Zusammensetzung der Epidote und Vesu-
viane, 269.

H. G. de Claubry.—De la détermination dans les eaux naturelles ou
minérales des proportions d’acide carbonique ou sulphydrique libres
ou combinés avec les bases, 428.

—. ——1860. No.1. 1860.

P. A. Kehlberg.—Verzeichniss der Erdbeben welche in Tselenginsk
in den Jahren 1847-57 beobachtet worden, 303.

Nouveaux Mémoires de la Société Impériale des Naturalistes
de Moscou. Vol. xi. 1859. Vol. xii. 1860.

Vol. xiii. Livr. 1. 1860.

J. Auerbach und H. Trautschold.—Ueber die Kohlen von Central-
Russland, 1 (map and 2 plates).

Munich. Gelehrte Anzeigen. Vol. xlx.

A. Wagner.—Monographie der fossilen Fische des lithographischen
Schiefers, 9, 17.

Scherer.—Massanalytische Bestimmung von Hisenoxyd durch unter-
schwefligsaures Natron, u. s. w., 195.

A. Vogel.—Der Torf, seine Natur und Bedeutung, noticed, 257.

O. Buchner.—Die Feuermeteore, noticed, 561.

A. Wagner.—Ueber einige im lithograph. Schiefer neu aufgefundene
Schildkvdten und Saurier, 553.

Vol. 50.

A. Wagner.—Die Griffelziihner (Stylodontes), 81.

——. Ueber das Vorkommen eines fossilen Fisches, im Juradolo-
mite, 102.

Zur Charakteristik der Gattungen Sawropsis und Pachycormus
nebst ihren Verwandten, 209.

Von Kobell.—Ueber eine eigenthiimliche Siure, Diansaure, in der
Gruppe der Tantal- und Niobverbindungen, 377.

A. Wagner.—Vergleichung der urweltlichen Fauna des lithogra-
phischen Schiefers von Cirm mit den gleichnamigen Ablagerun-
gen im Frankischen Jura, 390.

Ueber die Verschiedenheit der Arten von Jehthyosaurus,

ee
.

412.

DONATIONS. 247

Munich. Sitzungsberichte d. k. bayer. Akad. d. Wissensch. zu Mun-
chen. 1860. Hefte i. 11. ii.

A. Wagner.—Ueber die Arten von Fischen und Sauriern, welche im
untern wie im obern Lias zugleich vorkommen sollen, 36.

-—--. Ueber fossile Fische aus einem neuentdeckten Lager in den
siidbayerischen Tertiargebilden, 52.

C. von Martius.—Denkrede auf J. F. L. Hausmann, 57. __

A. Wagner.—Ueber fossile Siiugthierknochen am Chimborasso,
330.

Abhandlungen d. math.-phys. Classe d. k. bayer. Akad. d.
Wissensch. Vol. vii. Part 3. 1860.

A. Vogel.—Ueber die Zusammensetzung eines Gletscher-schlammes
vom Dachsteine am Hallstadter See, 627.

A. Wagner.—Die fossilen Ueberreste von nackten Dintenfischen
aus dem lithographischen Schiefer und dem Lias des siiddeutschen
Juragebirges, 749 (plate).

Paris. Bulletin de la Société Géologique de France. Deux. Ser.
Vol. xvi. Feuil. 13-44. Janvier—Mai 1860.

F. Hochstetter.—Recherches géologiques faites 4 Tapaipoumamoa,
ile moyenne de la Nouvelle-Zélande, 193.

C. Puggaard.—Sur les calcaires plutonisés des Alpes Apuennes et du
Monte Pisano, 199.

J. Guillemin.—Explorations minéralogiques dans la Russie d’Europe,
252 (plate).

E. Dumortier.—Sur quelques fossiles recueillis prés de Dax (Landes),
241.

R. Thomassy.—Hydrologie du Mississippi, 242. ‘

Marcel de Serres.-—Des espéces perdues, et des races qui ont disparu
des lieux qu’elles habitaient primitivement, depuis ou avant notre
existence, 262.

A. Passy.— Sur la carte géologique de l’Oise, 269.

Ebray et J. Fournet.—Sur la production de Cristaux dans les roches
a Vétat subsolide, 275, 277.

Ed. Hébert.—Du terrain jurassique supérieur sur les cétes de la
Manche, 300.

A. Laugel.—Sur la Géologie du Département d’Eure-et-Loir, 316.

De Verneuil, Collomb, Triger, et Cotteau.—Sur une partie du pays
Basque Espagnol, suivie d’une description de quelques Echino-
dermes, 553 (plate).

G. Cotteau.—Sur le genre Heterocidaris, 378 (plate).

Ad. Chatin.—Sur V’eau minérale et la roche de Saxon en Valais,
381.

iim. Benoit.—Sur les terrains tertiaires entre le Jura et les Alpes,
387 (plate).

De Vibraye.—Sur la découverte d’un nouveau gisement de vertébres
a Chitenay (Loir-et-Cher), 413.

A. Boué.—Statistique méthodique des Sociétés savantes, &c., 421.

Th. Ebray.—Sur les dépéts 4 oolithes ferrugineuses du Département
de la Niévre, 422.

GHEE Sr Vétage néocomien du Département de la Haute-Marne,
425,

s 2

248

DONATIONS.

Paris. Bulletin de la Société Géologique de France (continued).

Ponzi.—Sur des ossements fossiles trouvés dans les travertins prés
de Tivoli et de Monticelli, 431.

G. Bergeron.—Sur la phosphorescence d’une variété de Lapis-Lazuli,
432.

A. Boué.—Sur la symmiétrie de la surface du globe, et sur l’épaisseur
de la crotite terrestre a différentes époques géologiques, 433.

De Binkhorst.—Sur les couches crétacées du Limbourg, 459.

Marquis de Vibraye.—Sur les ossements fossiles et une machoire
humaine trouvés dans les grottes d’Arcy-sur- Yonne, 462.

W. Swarsood.—Du Cérium oxydé, 478.

Ch. Lory.—Sur un gisement de Nummulites en Maurienne, 481.

J. Beaudouin.—Sur des silex taillés trouvés aux environs de Chatillon-
sur-Seine, 488,

Lartet.—Sur des os fossiles portant des empreintes attribuées a la
main de Vhomme, 492.

J. Gosselet—Sur des fossiles siluriens frouvés dans le Brabant
(Belgique), 495.

Marquis de Raincourt.—Sur un gisement de la partie supérieure des
sables moyens, 499.

V. Raulin,—Sur les Almyvros de la Créte, 504.

Th. Ebray.—Sur la composition géologique du sol des environs de
Macon, 507.

C. de Prado, de Verneuil, et J. Barrande.—Sur lexistence de la
faune primordiale dans la chaine Cantabrique, 516 (3 plates).

E. de Verneuil et Caux.—Sur des ossements fossiles et des silex
taillés trouvés dans la sabliére de Précy (Oise), 555.

A. Delesse.—Sur les pseudomorphoses, 556.

Hi. C. Sorby.—De l’action prolongée de la chaleur et de V’eau sur
différentes substances, 568.

H. C. Sorby.—Sur Vapplication du microscope a l’étude de la Géologie
physique, 571. ‘

J. Barrande.—Troncature normale ou périodique de la coquille dans
certains Céphalopodes paléozoiques, 573 (plate).

EK. Goubert.—Deux échantillons de marne blanche avee Cérites,
trouvés & Romainville (Seine), 600.

J. Barrande.—Colonies dans le bassin silurien de la Bohéme, 602.

R. Thomassy.—Sur Vhydrologie maritime et sur les lignes d’équisa-
lure de Pocéan Atlantique, 666.

Anca.—Sur la découverte en Sicile de deux nouvelles grottes 4 osse-
ments fossiles, 680, 684 (2 plates).

Th. Ebray.—Sur le mode de formation des poudingues de Nemours,
693.

Sur la conséquence du principe de surdissolution, 697.
Michel.—Coupe du terrain silurien aux environs de Domfront (Orne),
698.

——. Comptes Rendus hebdom. des Séances de Acad. des Sciences.
Vol. Go Nios =i lOO:

= See, lS Trim Wrame UEG0A Walk AiO).

Voizot.—Considérations sur l’origine de l’univers, tirées de la Note
vil. et derniére de l’Exposition du ‘Systéme du Monde’ de Laplace,
1033.

Sorby.—De action prolongée de la chaleur et de l’eau sur diverses
substances, 990.

DONATIONS. 249

Paris. Comptes Rendus. Tables. Vol. 50 (continued).

Aulagmer.—Action dissolvante des eaux sur les calculs, 149.

Caillat.—Sur un procédé particulier d’application des eaux minérales
usité aux bains d’Hercule en Hongrie, 684.

Jackson.—Découverte dun bloc de fer météorique dans l’Oregon
(Htats-Unis d’Amérique), 105.

R. I. Murchison.—Nouvelle classification des anciennes roches du
nord de l’Kcosse, 715.

Fournet.—Sur un faille s’étendant de Vile de la Galite a la mine de
Kef-Oum-Theboul en Algérie, 902.

Sur la diffusion d’une matiére organico-minérale, et sur son
role de principe colorant des pierres et des roches, 1175.

Elie de Beaumont.—Sur une recrudescence des phénoménes volca-
niques et des tremblements de terre; éruption du volcan de Vile
de la Réunion ; tremblement de terre & Saint-Domingue, 899.

Palmieri.—Sur l’état actuel du Vésuve, 726.

Liais.—Inclinaison des couches de roches arénacées modernes des
cotes du Brésil, 762.

Beautemps et Miliner.—Fragment de roche détachée du grand bane
de Terre-Neuve, 824.

Anca.—Découverte en Sicile de deux nouvelles grottes 4 ossements
fossiles, 1139, 1203.

Guiet.—Sur les derniéres révolutions du globe, 448.

Delesse.—Recherches sur les pseudomorphoses, 944.

Marignac.—Sur la formule de la zircone, 952.

Cappa.—Analyse chimique de deux variétés de Cotunnite recueillies
apres l’éruption du Vésuve de 1858, 955.

Damour.—Examen minéralogique et analyse chimique d’un pétrosilex
glanduleux recueilli par M. Elie de Beaumont sur la pente des
Coevrons (Sarthe), 989.

Lartet.—Sur Vancienneté géologique de Vespéce humaine dans
V’Europe occidentale, 599, 790.

Gosse.—Sur des silex taillés trouvés 4 Paris, 812.

Gaudry.—Sur les plantes fossiles de ’Eubée, 1093.

A. Sismonda.—Sur un nouveau gisement de fossiles jirassiques des
Alpes, 1190.

Secchi.—Sur le tremblement de terre qui le 22 aotit a détruit la ville
de Norcia, 377.

Prost.—Sur les trépidations du sol dans une partie de la ville de
Nice, 596.

Durocher.—Sur l’orographie et la géologie de ’ Amérique centrale,
1170.

A. Vezian.—Sur les systémes de la Margeride et des Vosges, re-
spectivement perpendiculaires & ceux du Hundsruck et des
Ballons, 89.

Sur les mouvements généraux de l’écorce terrestre, 814.

Omboni.—Sur les terrains sédimentaires de la Lombardie,

Lorry et Pillet.—Sur la présence de Nummulites dans certains grés
de la Maurienne et des Hautes-Alpes, 187.

Méne.—Sur certains schistes calcaires des montagnes du Bugey,
445.

Simonin.—Sur les gisements auriféres de la Californie, 889.

Scipion Gras.—Sur l’opposition que l’on observe souvent dans les
Alpes entre ordre stratigraphique des couches et leurs caractéres
paléontologiques, 754.

Marcel de Serres.—Sur les dépots récents des cotes du Brésil, 907.

250 DONATIONS.

Paris. Comptes Rendus. Tables. Vol. 50 (continued).
Marcel de Serres.—Coprolites des terrains tertiaires éocénes des en-
virons d’Issel (Aude), 1086.
Sur la classification des métaux d’Haiiy, 167.
—. Nouvel ordre a établir parmi les substances métalliques, 324.

Comptes Rendus hebdom. des Séances de l’Acad. des Sciences.
Vol. xh. Nos. 18-22. 1860.

Mémoires de l’Acad. des Sciences de l'Institut Impérial de
France. Vol. xxx. 1860.

Photographic Society. Journal. Nos. 103, 104.

Rio de Janeiro. Revista Brazileira. Jornal de Sciencias, Lettras
e Artes, dirigido por Candido Baptista de Oliveira. Numero 4.
Jan. 1859. From Sur C. Lyell, V.P.G.S.

C. B. de Oliveira.—Memoria sobre as condigdes geologicas do porto
do Rio de Janeiro, 57 (map).

F. L. C. Burlamaque.—Noticia acerca de alguns mineraes e rochas
de varias provincias do Brazil, recebidos in Muséo Nacional du-
rante o anno de 1855, 73 (plate).

Se NO OU SeLEMp aLCOO:

Boussingault.—Da terra vegetal considerada em sens effeitos, 369.
Royal Institution of Great Britain. List of Fellows, &e. 1860.
——. Additions to the Library. From July 1859 to July 1860.

Notices of the Proceedings. Part 10. Nov. 1858—July
1860.

F. Field.—The Mineral Treasures of the Andes, 190.

T. H. Huxley.—Species and Races, 195.

N. S. Maskelyne.—Diamonds, 229.

W. Pengelly.—Devonian Fossils, 265.

Royal Geographical Society. Proceedings. Vol. iv. No. 5.

Royal Society. Proceedings. Vol. x. No. 41.
J. H. Pratt.—Curvature of the Indian Are, 648.

St. Petersburg. Bulletin de l’ Acad. Imp. des Sc. de St.-Pétersbourg.
Vol. ii. Nos. 1-3. 1860.

K. E. Bauer.—Sur une loi générale de la formation du lit des rivieéres,
1, 218.

A. de Middendorff{—Lvile d’Anikief dans la mer Glaciale, prés de
Kola, 152.

C. Claus.—Sur les métaux qui accompagnent le platine, 158.

J. F. Brandt.—Sur un squelette de Mastodon, trouvé prés de Niko-
laief, 193.

DONATIONS. 251

St. Petersburg. Mém. de l’Acad. Imp. des Se. de St.-Pétersbourg.
6me Série. Sc. Math., Phys. et Nat., Vol. ix. Prem. Part. Sc. Math.
et Phys., Vol. vii. 1859.

H. Abich.—Vergleichende chemische Untersuchungen der Wasser
des Caspischen Meeres, Urmia- und Van-See’s, 1 (2 plates).

Ueber das Steinsalz und seine geologische Stellung im rus-
sischen Armenien, 59 (11 plates).

A. v. Kokscharow.—Ueber den russischen Phenakit, 175.

G. v. Helmersen.—Geognostiche Bemerkungen auf einer Reise in
Schweden und Norwegen, 293 (3 plates).

H. Abich.—Vergleichende Grundziige der Geologie des Kaukasus,
wie der armenischen und nordpersischen Gebirge, 359 (8 plates).

——. Beitrage zur Palaontologie des asiatischen Russlands, 555
(8 plates).

——. ——. Vol. x. See. Part. Sc. Nat., Vol. viii. 1859.
——. ——. 7meSérie. Vol. ii. Nos. 4-7. 1860.

INGevs Kokscharow. —Anhane zu der Abhandlung “‘iiber die russi-
schen Topase.”

M. v. Griinewaldt.—Beitrage zur Kenntniss der sedimentiaren Ge-
birgsformationen in den ‘Ber oehauptmannschaften Jekathermburg,
Slatoust und Kuschwa (6 plates).

Society of Arts. Journal. Vol. viii. Nos. 415-425.
G. R. Burnell.—Preservation of Stone, 830.
Consular Information, 77, 90.

Stockholm. Kongl. Svenska Vet.-Akad. Maj 1860. Beskyddare
hans maj. t konungen. Féorste heders-ledamoter, &c.

Kong. Svenska Vet.-Akad. Handlingar. Ny Foljd. Andra
Bandet. Andra Haftet. 1858.

Ofversigt af Kongl. Vetenskaps-Akad. Forhandlingar. Sex-
tonde Argangen. 1859.

Hultmark.—Chrysotil och Serpentin fran Sala, 282.
Igelstrém.—Stilpnomelan och Pektolit 1 Sverige, 399.
Lilj eborg.—F ynd af fossilt Hvalskelett, 327.

Nor deneliold! —Gadolinitens kristallform, 287.
Nylander.—Qvicksilfer-cyanid- dubbelsalter, 281.

Turin. Memorie della Reale Accademia delle Scienze di Torino.
Serie Seconda. Vol. xviii. 1859.

M. Levi.—Sopra una nuova lega cristallizzata di Nichelio e Ferro,
lyiii.

HE. Sismonda.—Prodrome d’une Flore tertiaire du Piémont, 519,

252 DONATIONS.

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 8rd Series, Vol. vi.
Nos. 35 and 36. Nov. and Dec. 1860.

W. K. Parker and T. R. Jones.—Nomenclature of the Foraminifera
Denys de Montfort’s Species, 337.

A. Gray.—The Origin of Species, 373.

R. Damon’s ‘ Handbook to the Geology of Weymouth and Portland,’
noticed, 436.

G. C. Wallich.—Deep-sea Soundings in the North Atlantic, 457.

Leonhard und Bronn’s Neues Jahrbuch fir Min., Geol. u. s. w.°
Jahrgang 1860. Fiunftes Heft.

Schlonbach.—Das Bone-bed und seine Lage gegen den sogen. obern
Keupersandstein im Hannoverschen, 515 (plate).

F. Scharffi—Ueber die milchige Trubung auf der Endflaiche des
siuligen Kalkspaths, 535 (2 plates).

Letters: Notices of Books, Minerals, Geology, and Fossils.

Ill. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italics.
Archiac, A. d’. Notice sur la vie et les travaux de P.-A. Dufrénoy.
From Sir R. I. Murchison, V.P.G.S. 1860.
Berger, H. A. C. Die Versteinerungen der Fische und Pflanzen im
Sandsteme der Coburger Gegend. 1832. From Sw C. Lyell,
VP: Gast

——. Die Verstemerungen des Schaumkalks am Thiringer Wald.
1860. From Sir C. Lyell, V.P.GS.

——. Die Verstemerungen im Roth von Hildburghausen. 1859.
From Six C, Lyell, V.P.GS.

Bland, T. Remarks on certain species of North American Helicide,
with descriptions of new species. 1860.

Bouquet. Nouvelle analyse de l’eau de la source de Saint-Yorre,
Bassin de Vichy. 1860.

Brandt, J. F., und G. v. Helmersen. Vorschlag zur Anstellung
paliontologischer Nachgrabungen im siidlichen Russland. 1860.

Carpenter, W. B. Researches on the Foraminifera. Part III.
On the Genera Peneroplis, Operculina, and Amphistegina. 1858.

bat

DONATIONS. 253

Clarke, W. B. Researches in the Southern Gold-fields of New
South Wales. 1860.

Cooke, J. P. Crystalline Form not necessarily an indication of
definite chemical composition ; or on the possible variation of con-
stitution in a mineral species independent of the phenomena of
Isomorphism. 1860. rom Sir C. Lyell, V.P.GS.

Daubrée, A. Etudes et expériences synthétiques sur le Métamor-
phisme et sur la Formation des roches cristallines. 1860.

Dawson, J. W. Notes on the Earthquake of October 1860. 1860.
——. Supplementary Chapter to ‘‘ Acadian Geology.” 1860.

Deville, C. Ste.-C. Lettre 4 M. Dumas sur quelques produits d’éma-
nations de la Sicile. 1855. From Sir C. Lyell, V.P.GS.

Lettres 4 M. HE. de Beaumont sur l’éruption du Vésuve du
le Mai 1855. 1855. From Sur C. Lyell, V.P.GS.

Lettres 4 M. E. de Beaumont sur les phénoménes éruptifs du
Vésuve et de l’Italie méridionale. 1856. From Sir C. Lyell,
VEEAGS:

et F. Leblanc. Mémoire sur la composition chimique des
Gaz rejetés par les évents volcaniques de l’Italie méridionale.
1859. From Sir C. Lyell, V.P.G.S.

Evans, J. On the Flint flakes and implements from Reigate. 1860.

Falconer, H., and H. Walker. Descriptive Catalogue of the Fossil
Remains of Vertebrata from the Sewalik Hills, the Nerbudda,
Perim Island, &c.,in the Museum of the Asiatic Society of Bengal.
1860. From the Asiatic Socety of Bengal.

Gemitz, H. B. Der Gebirgsbau Sachsens und sein Hinfluss auf das
Studium der Naturwissenschaften in Dresden. 1860. °

Geological Survey of Canada. Report of Progress for the year 1858.
1859. From the Geological Survey of Canada.

Halloy, J.J. VO. dad. Notice biographique sur Alexandre Bron-
eniart. 1860. From Sw Rk. I. Murchison, V.P.GS.

Helmersen, G.v. Beschreibung einiger Massen gediegenen Kupfers,
die aus russischen Bergwerken herstammen, und in dem Museum
des Berginstituts zu St. Petersburg aufbewahrt werden. 1859.

Jeffreys, J.G. Sui Testacei Marini delle Coste del Piemonte. Tra-
duzione, con note ed un catalogo speciale per il Golfo della Spezia,
del Prof. G. Capellini. 1860. From Sir C. Lyell, V.P.GS.

Jones, T. R., and W. K.Parker. On some Fossil Foraminifera from
Chellaston, near Derby. 1860.

ae DONATIONS.

Koettig, R. F. Geschichtliche, technische und statistische Notizen
uber den Steinkohlen-Bergbau Sachsens. 1861. From Prof. Dr.
Gemnitz, For.M.GS.

Kongliga Svenska fregatten Eugenies Resa omkring Jorden, under
Befal af C. A. Virgin, aren 1851-538. Zoologi, IV. 1859. From
the Royal Academy of Stockholn,

Lane, C. B. Railway-communication in London, and the Thames
Embankment. 1860.

Lieber, 0. M. Report on the Survey of South Carolina ; being the
Fourth Annual Report, &c. 1860. From Sur C. Lyell, V.P.G.S.

Martius, C. F. P.v. Denkrede auf Alexander von Humboldt. 1860.

Miller, M. J. Kinleitende Worte zur Feier des Allerhochsten Ge-
burtsfestes Sr. Majestat des Konigs Maximilian IT. 1859.

Nisser, P. On the Elementary Substances originating and promoting
Civilization through the World. 1860. From Sir C. Lyell, V.P.G.S.

Parker, W. K., and T. R. Jones. On the Nomenclature of the Fora-
minifera. Part 5. The Species enumerated by De Montfort. 1860.

Passy, A. Notice biographique sur M. Louis Graves. 1860: From
Sir R. I. Murchison, V.P.G.S.

Phillips, John. Wife on the Earth, its Origin and Succession. 1860.

Puggaard, C. Mémoire sur les calcaires plutonisés des Alpes Apu-

ennes et du Monte Pisano. 1860. From Sir R. I. Murchison,
Mnlen CS Sr

. Notice sur les calcaires plutonisés de la péninsule de Sorrento.
1859. From Sir R. I. Murchison, V.P.GS.

Reeve, L. Elements of Conchology. Parts15 &16(inone). 1859.

Reentzsch. Die Pechsteime des Meissner Porphyr-Districts. Einla-
dungsprogramm zu den offentlichen Priifungen an der I. Realschule
zu Neustadt-Dresden. 1860.

Scharff, F. Ueber die milchige Trubung auf der Endflache des sau-
ligen Kalkspaths. 1860.
——. Werner und R. Delisle in Zusammenstellung mit Haiiy. 1859.

Sorby, H. C. De Vaction prolongée de la chaleur et de l’eau sur
différentes substances. 1860.

Wallich,G.C. Notes on the presence of Animal Life at vast depths
in the Sea, with observations on the nature of the sea-bed, as
bearing upon Submarine Telegraphy. 1860.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

Frsruary 15, 1861.
Annuat Generat MEETING.

[For the Reports of the Council and Anniversary Address, see the beginning of
this Volume. |

Frsrvary 20, 1861.

J. Frederick Davis, Esq., Walker Iron-works, Newcastle-upon-
Tyne ; John Frederick Collingwood, Esq., 13 Old Jewry Chambers ;
Joseph Milligan, Esq., F.L.S., Hobart Town ; Henry Porter, M.D.,
Fellow of Queen’s College, Birmingham, Peterborough ; and Richard
Charles Oldfield, Esq., Bengal Civil Service, Farley Hill, Reading,
were elected Fellows.

The following communications were read :—

1. On the Cotncrprence between the Srratrrication and Forratron of
the AutERED Rocks of the Scorrisn Hrenianps. By Sir Roprrtcx
I. Murcutson, V.P.G.8S., F.R.S., &e., and A. Germin, F.GS.,
F.R.S.E., &e.
[See above, page 232. ]
VOL, XVII.—PART 1. T

256 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

2. On the Rocks of Portions of the Hicuianns of Scottanp Souru
of the CALEDONIAN Canali; and on their Equivaents in the Norra
of Iretanp. By R. Harkness, F.R.S., F.G.8., Professor of
Geology in Queen’s College, Cork.

ConTENTS.
§ 1. Introduction. § 7. Sections N.W. of the great zone
§ 2. Section from Callender to Loch of quartz-rocks and limestones.
Earn. Section from Glen Lyon to Loch
§ 3. Section from Loch Earn to Loch Treig.
Tay. § 8. Section from King’s House
§ 4. Section from Loch Tay to Glen through Glencoe to Baliahu-
Lyon. lish.
§ 5. Section from Dunkeld to Blair | § 9. Section across the peninsula of
Athol. Ardsheal from Benivair.
§ 6. Sections from the south side of | § 10. Metamorphic rocks of the County
Ben-y-Gloe Mountains and of Donegal, and section of the
Strath Ardle. east side of Lough Foyle.

$ 1. Introduction.—The recent labours of Sir Roderick Murchison
in the N.W. Highlands of Scotland have so greatly increased our
knowledge of this portion of Great Britain, as to place the age and
arrangement of the rocks in this country in an entirely new aspect.
The result of these investigations has been made known so lately *
that it must be visibly impressed on the mind of every geologist,
and consequently will require no special reference to be made
thereto. In the memoirs in which these labours have been de-
tailed, there is a ‘‘ hypothetical view ” expressed concerning the
mass of metamorphic rocks which constitute the great bulk of the
Scottish Highlands; and in this hypothetical view these rocks are
looked upon as the equivalents of the “upper gneiss” found re-
posing upon the quartz-rocks and limestones of Assynt and Dur-
ness, and which occupies so large a portion of the north of Scot-
land.

Having had an opportunity of examining the deposits of Suther-
land so amply described by Sir Roderick Murchison, and cor-
roborating the results of his labours in the N.W. Highlands, I have
felt myself in a position which has enabled me to extend to a more
southern parallel investigations concerning the great area of Scot-
tish metamorphic rocks, and, as will be seen in the sequel, from
observations made last summer in many parts of the Highlands,
and also in the north of Ireland, have arrived at the same con-
clusions as are expressed in the hypothetical views already re-
ferred to.’

Before proceeding to detail the results of these observations, it is
necessary to say something concerning the nature of the rocky
masses which abound in the more southern part of the Highlands,
more especially as these are laid down in the geological maps of
this district. Certain rocks, to which the term metamorphic is
usually applied, have had assigned to them somewhat definite areas

* See Quart. Journ. Geol. Soc., vol. xvii. p. 252 &c., as well as other previously
published memoirs.

1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. 257

in the Highlands; and these rocks, generally designated gneiss,
mica-slate, chlorite-slate, and clay-slate, have been looked upon as
possessing a distinct arrangement as to superposition to each other.
From what I have seen in the several areas which have been under
my examination, it appears to me that these rocks, with names ex-
pressing lithological nature, have no definite relation as concerns
geological position, although in some small areas this seems to be
the case. Looking at these metamorphic rocks with reference to
general results, I have arrived at the conclusion that, in whatever
mineral condition they present themselves, this mineral condition
is a purely local character, and that, in the same geological zone,
in one spot we have clay-slate, in another chlorite-slate, in a
third mica-slate, and in a fourth gneiss. These several rocks are
altered deposits of varying shales and sandstones which were de-
posited during the same period in different portions of the older
Silurian seas. These metamorphic rocks, to which I apply the
general term “ gneissose,” although the word is in many instances a
bad one, are spread over too great an extent in the geological maps
of Scotland ; and they are frequently represented as occupying large
areas, over which granite or some other form of plutonic rock
really prevails. And, although rocks of the latter nature seem to
be so amply developed in the Highlands, great injustice is in many
instances done to rocks of this description in the geological maps of
Scotland.

With reference to the mode of arrangement of the other strata
which are associated with the gneissose rocks (viz. the quartz-rocks
and limestones), it has generally been assumed that these latter
occupy a higher position than the former. This inference I have
reason to conclude is not the result of observation, but has ori-
ginated from the Wernerian theory and classification of rocks,—the
more crystalline gneissose rocks having been looked upon as primi-
tive, while the less crystalline and more distinctly stratified quartz-
rocks and limestones were regarded as transition. This idea appears
to have prevailed in the mind of Macculloch ; and this order, in the
arrangement of the stratified masses of the Highlands propounded
by him, has been to a great extent adopted by geologists without
inquiring into the basis on which it rests.

The principles which actuated Macculloch in his classification of
the Highland rocks may be ascertained by referring to his memoir
“on Quartz-rock,” where, after quoting Playfair with reference to
the structure of Schihallien, he goes on to say, “If this ridge is
connected by any system of alternation with the sandstone of Glen
Lyon, mica-slate will appear to be a rock formed posteriorly to, or
alternately with, a rock of recomposed structure. Thus a primitive
will be found to alternate with a transition one,—an anomaly which
either renders this distinction as useless as it is artificial, or compels
us to modify the definition of transition rocks or to form that total
change of arrangement which I have more than once suggested with
regard to primitive and transition classes*.”

* Geol. Trans., vol. ii. p. 470.

t 2

=

258 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

Again, in the same memoir, with reference to Jura, alluding to
the gheissose rocks, he states that these are “apparently super-
imposed on the quartz-rock* ;” and yet, after using the word appa-
rently as though this was not the true position, he goes on (at p. 456)
to quote Prof. Jamieson, who says that ‘‘ quartz-rock rises at an
angle of 45° from under micaceous schists.”

The same idea as to primitive and transition seems to have been
the leading feature in his mind with relation to arrangement when
he visited Glen Tilt; and yet, when he comes to describe definitely
the sequence of rocks here, we generally find that his statements
are hostile to his preconceived ideas.

These general observations will serve as a prelude to what I
have to add to the geology of portions of the Highlands lying south
of the Caledonian Canal; and, as these ahyernsone have reference
to purely physical geology, I shall proceed to describe the several
sections, and afterwards the general results obtained therefrom.

Fig. 1.—Section from Callender to Loch Earn. Distance 9 miles.
* Callender. Woodhead. Anneehaugh. Ardchullarie. Ruskin Burn.

e asd” d d Cignnha:
e. Old Red Sandstone. d. Gneiss. c. Limestone. 6. Shale.
a. Quartz-rock. * Trap-rocks.

§ 2. Section from Callender to Loch Earn (fig. 1).—In the imme-
diate neighbourhood of Callender, deposits belonging to the Old Red
- Sandstone series are extensively developed. At the distance of
about a mile and a half to the N.W. of the village, the great
line of fracture separating the rocks of this age from the meta-
morphie strata of the Grampians is seen. In Leny Glen the point of
contact between the rocks appertaining to these different series 1s ex-
hibited, the rocks of the Old Red series appearing in the form of
conglomerates ; immediately on the N.W. of them, above the line
of fault, quartz-rocks, referable to the older deposits, occur; and
upon the small development of the quartz-rocks here seen, black
shales are found reposing conformably. These quartz-rocks and
black shales dip towards the N.N.W. On leaving this glen and
continuing the section on its rise, we have, at Leny lime-quarry,
the same black shales manifested, dipping N.N.W. at 35°, and
possessing an anthracitic aspect, which allies them in lithological
nature with the anthracitic shales of the Lower Silurians of the
South of Scotland. In these black shales, which from their nature
might have afforded abundance of Graptolites, no fossils were ob-
tained. Resting conformably on these shales, a thin layer of lime-
stone is seen, of a dark grey colour, regularly bedded, but contorted,
and abounding in white veins of carbonate of lime. This limestone,
which also afforded no fossils, and which has a thickness of about
eight feet, is succeeded by grey clay-slate, in some instances wea-

* Geol. Trans., vol. ii. p. 454.

1861. | HARKNESS—HIGHLANDS AND N. IRELAND. 259

thering to a purple colour, and with gneissose layers intercalated
init. This latter mass is conformable to the limestone ; and, pass-
ing upwards into regular mica-slate, it forms the hills which lie
N.W. of Leny lime-quarry. On the road from Callender to Loch
Lubnaig, at Woodend, about half a mile from Kiimahog toll-bar,
quartz-rocks, similar to those of Leny Glen and having the same
inclinations, appear. The succeeding black shales and limestones
are not seen, being masked by débris, but the overlying purple
shales occur, passing into gneissose rocks; and these are intersected
by a trap-dyke, termed locally “ Blue Whin,” at Woodhead Quarry.

The arrangement of the rocks forming a portion of the southern
boundary of the metamorphic masses of the Highlands, as seen in
the neighbourhood of Callender, is exhibited in fig. 1, and is as fol-
lows :—First and lowest, quartz-rock, a small portion only of which
is exhibited; second, black shales; third, thin grey limestones ;
and fourth, clay-slates (shales) passing into gneissose rocks.

Beyond the Woodhead whin-quarry we have a considerable
development of that form of metamorphic rock to which the name
chloritic schist has been applied, but of which the term “ chloritic
gneiss of a fine grain” more fully expresses its nature; and this
rock continues with the same N.W. dip to Anneehaugh, about three
miles from Callender, where it is intersected by another trap-dyke
containing red nodules. North of this dyke the same chloritic gneiss
is seen dipping in the same direction, but at angles varying from
40° and upwards, until we reach Ardchullarie, where another trap-
dyke makes its appearance ; and to this the name “ Black Whin” is
applied. These trap-dykes produce very little effect on the dip of
the metamorphic rocks. After leaving Ardchullarie, we find that
northward the strata become much disturbed, and show a dispo-
sition to assume 8.E. dips. At Creggan, about half a mile north of
Strathire village, this 8.E. dip is very apparent. At Ruskin Burn
another trap-dyke occurs, and also a vein-like mass of limestone
very thinly overlain by gneiss, the latter dippmg N.E. ‘There is a
considerable amount of disturbance in the strata here, and northwards
this disturbance also prevails. This mass of gneissose rocks occur-
ring in the area between the hills of Leny and Loch Earn, and
which possesses a great thickness, overlies the limestones of the
southern margin of the Grampians ; and, notwithstanding its flexures
and contortions, clearly arranges itself as a synclinal axis in the
neighbourhood of Strathire village, from underneath which we have
limestones making their appearance at Leny on the 8.S.E., and at
Ruskin Burn on the N.N.W. The mode of arrangement of the
rocks in this interval is shown in fig. 1.

§ 3. Section from Loch Earn to Loch Tay (fig. 2).—At the N.W.
end of Loch Earn, at Dall, a considerable mass of limestone, having
somewhat of a gneissose aspect, and exhibiting itself in great thick-
ness, is seen. This limestone at this locality is nearly horizontal ;
but at the east side of the quarry, where it has been wrought, it
inclines at a low angle towards the E.S.E., and is succeeded by
chloritic gneiss. Near the seventh milestone from Killin, at Loch

260 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Feb. 20,

Earn head, this same gneiss also makes its appearance, dipping in
the same direction at an angle of 20°; and at the bridge, about a
mile north of Loch Karn head, a hard trap occurs, from which the

Fig. 2.—Section from Loch Earn to Loch Tay, Distance 6 miles.
s. N

Dall. Glen Ogle. Larigellie Loch. Dochart River.
1 i <i i f

: WX E
~~ =
i YS

x =

c d d c d
d. Gneiss. ec. Limestone. x Trap-rocks.

metamorphic strata seem to derive the E.S8.E. inclination. On the
north side of this mass of trap, which is much intersected by quartz-
veins, a reversed dip is seen and N.W. inclinations obtain.

Along Glen Ogle, the gneiss, which is micaceous, is only slightly
inclined, and has quartz-veins running along the lines of stratifi-
cation. At Larigellie Loch, a small lake near the water-shed of
Glen Ogle, the E.S.E. dips become most prevalent; and these con-
tinue to the shepherd’s cottage, where limestone again occurs,
dipping at an angle of about 40° E.S8.E. This limestone is seen along
the course of the Larigellie Burn, where it becomes flattened; and
at the bridge, where the high road crosses this stream, about a mile
and a half from Killin, another mass of trap makes its appearance.
In the arrangement of the strata in the section between Loch Earn
and Loch Tay, we have a mass of limestone near Loch Earn which
underlies the gneissose rocks, and near Loch Tay gneissose rocks
are seen, superimposed also in limestone. This limestone, as seen
in the Larigellie Burn, seems to form a rounded anticlinal; for,
immediately on its north side, we have gneissose rocks amply deve-
loped in the River Dochart, and these dip N.W. at an angle of 20°,

§ 4. Sections from Loch Tay to Glen Lyon (fig. 3).—The rocks just
referred to, as seen in the Dochart, also appear on the road from

Fig. 3.—Section from Loch Tay to Glen Lyon. Distance 9 miles.
s

; N.
Loch Tay. Loch-a-Larich, Glen Lyon.

d. Gneiss. c. Limestone. a. Quartz-rock. f. Fault.

Killin to Lochie Bridge, and for a short distance along the road to
the eastward, having the same N.W. inclination. About half a
mile east of Lochie Bridge strata of limestone occur, having thin
bands of rotten gneiss interstratified; the limestone is also thin-
bedded. These limestones dip N.N.W. at 60°. At Mornish,
about two miles east from Killin, similar limestones also occur.
They have, however, a gneissose aspect, and are greatly con-
torted ; ‘but still the prevailing dip (N.N.W.) of this portion of

‘ =
1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. 261

the Loch Tay rocks obtains. To the south of these contorted lime-
stones at Mornish, a flaggy trap is seen. ‘These limestones of the
north side of Loch Tay are well exhibited for a considerable di-
stance along their strike, on the road leading from Killin to Ken-
more. They are well seen on their dip in traversing the mountain-
road from Loch Tay to Inverwick in Glen Lyon; and also in the
streams which run nearly parallel to this mountain-road, which in-
tersect the valleys lying between Ben Lawers on the east, and Meal
Girdy on the west. The section which is shown in this traverse
between Loch Tay and Glen Lyon, is probably one of the most
instructive which can be seen in any part of the Grampians south
of the Caledonian Canal. Commencing near the north margin of
Loch Tay, we have the thin-bedded limestones with their N.N.W.
dips succeeded conformably by gneiss; but this gneiss becomes
much contorted in the neighbourhood of Loch-a-Larich ; still the
prevailing N:N.W. dip is seen. After passing the water-shed, a
reversed dip in this gneiss occurs; and these reversed §.8.E. dips
are well seen in the rocky course of the brook which has its origin
on the N.E. side of Meal Girdy. These gneissose rocks, which are
seen in almost constant succession for more than two miles and a
half along this stream, have a S.S.E. dip, which averages 45°.
Then, as we approach Glen Lyon, we find coming out conformably
beneath the gneiss limestones like those of the north side of Loch
Tay ; and after passing downwards through the limestones, we find
underneath them, and also conformable to them, the thick masses
of quartz-rocks which are so extensively developed along the south
side of Glen Lyon. After crossing this area in a northern direction
to Inverwick, we find the quartz-rocks suddenly disappear, and on
their N.W. side we have thin-bedded blackish gneissose rocks with
the same §8.8.E. dips; and rocks of this character are well seen in
the course of the burn leading from Inverwick to Dall, on the south
shores of Loch Rannoch. Reference will subsequently be made to
this gneiss when describing the sections which lie N.W. of the
zone marked in Sir Roderick Murchison’s sketch-map* of the geology
of the north of Scotland, as occupied by “ quartz-rock and lime-
stones.”

§ 5. Section from Dunkeld to Blaw Athol (fig. 4).—In portions of
the Grampians which lie N.E. of the areas already referred to, we
have sections which are very nearly allied to those already de-
seribed. In many instances, in these north-eastern areas, the rocks
are by no means so well exposed as in the districts which have
been under previous notice. In the neighbourhood of Dunkeld the
relations of the Old Red Sandstone deposits to the metamorphic
rocks of the Grampians are well seen,—the former being cut off
from the latter by masses of trap, and the metamorphic strata
marked by the N.W. dips which distinguish the southern margins
of this class of rocks. With reference to lithological character, we
have at Dunkeld schistose beds, possessing the nature of clay-slates,
as the lowest exposed rocks of the metamorphic series ; and these

* Quart. Journ. Geol. Soc., vol. xv. pl. 12.

262

N.N.W.

Distance 20 miles.

Section from Dunkeld to Blair Athol.

Fig. 4.

S.S.E,

Blair.

Pitlochrie.

Moulinearn,

Dunkeld.

Killiecrankie. Essangeal.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

* Trap-rock.

c, Limestone.

d. Gneiss.

e. Old Red Sandstone.

are succeeded by micaceous schists pass-
ing upwards into gneiss. This must, as
already mentioned, be regarded only as
a local circumstance. After leaving
Dunkeld for the N.W., the valley of the
Tay becomes so expanded that the ex-
hibitions of rocks are by no means fre-
quent. On approaching Moulinearn we
find indications of a reversed dip pre-
vailing among the gneissose strata; but
on reaching Pitlochrie at the bridge over
the Tummel, a N.N.W. dip obtains; and
near this we have limestones very abun-
dantly developed, inclining at an angle
of 35°. The Pitlochrie limestone has a
somewhat gneissose appearance, and is
to a considerable extent made up of
layers of a grey and a white colour, the
latter resulting from the deposition of
more crystalline carbonate of lime in the
hollows produced by the opening of the
lamine consequent on flexures and con-
tortions.

This limestone at Pitlochrieinits na-
ture has great affinity to that on the
north side of Loch Tay; and there is,
from its line of strike, strong reason to
regard it as an extension north-east-
ward of the Loch Tay beds.

At Craigeoch, about a mile N.W.
from Pitlochrie, we have gneissose rocks
coming on; and these, dipping at 70°
N.N.W.., represent the rocks of the same
character which have been described
as succeeding the limestones of Loch
Tay in the section from this loch to Glen
Lyon. Continuing the section north-
westwards, we have, in the neighbour-
hood of the Pass of Killiecrankie, re-
versed or S.E. inclinations among the
eneissose rocks; and at Essangeal a
thick grey limestone, with imperfect
bedding, and seeming to dip under the
gneissose strata, appears. Between Es-
sangeal and Blair no rocks are exhibited
on the road; but at the latter spot we
have the limestone again shown with a
S.E. dip. This limestone of Blair I re-
gard as the same as that seen at Essan-
geal, and that its appearance here is the

1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. 263

result of one of those contortions, exceedingly common in the rocks of
more eastern parts of the Highlands, which have originated from the
influence of those great masses of plutonic rocks so abundant in these
portions of the Grampians.

§ 6. Sections from the South Side of Ben-y-Giloe Mountains and
Strath Ardle (fig. 5).—On leaving Blair and passing in the direction
of the southern flanks of the Ben-y-Gloe Mountains, a moory area is

Fig. 5.—Section from Ben-y-Gloe Southward. Distance 3 miles.
Ss. Gairnog. Ben-y-Gloe. N,
at

ad ¢ d ¢ a
d. Gneiss. c. Limestone. a. Quartz-rock.

traversed, which affords at irregular intervals exposures of dark-
coloured gneiss, dipping 8.E., or from the Ben-y-Gloe range. This
eneiss is well seen in the course of the Gairnog stream, which enters
the Gary near Killiecrankie. At the shepherd’s house near this stream,
on the road over the hills from Blair into Strath Ardle, these gneissose
rocks dip 8.E. at 45°, and are seen overlying limestone. To the
north of this parallel of limestone, black gneiss again occurs, having
the same inclination, and is found reposing on limestones which are
well seen in the escarpments which lie between the small Loch
Vallean on the south and the Ben-y-Gloe Mountains on the north.
The relations which these limestones bear to the quartz-rocks of the
Ben-y-Gloe Mountains are not seen, as the sides of the latter moun-
tains afford only débris of quartz-rocks, and along the stream-
courses which drain their south flanks, no exposures of rock in situ
are visible. It is probable that the connexion between the lime-
stones and the quartz-rocks of Ben-y-Gloe is cut off by plutonic
masses ; for we find the water-shed which separates the Gairnog from
Alt-Clunie, a stream flowing into Strath Ardle, to be composed of
coarse-grained syenite; and rocks of a plutonic character are exten-
sively developed along the southern margins of the great mass of
quartz- rocks which occur in this portion of the Highlands, although
no indications of such rocks are laid down in any geological map of
this portion of Scotland. From Alt-Clunie, below the syenitic area,
gneissose rocks occur, inclined at a very high angle towards 8.8.E.
These soon become perpendicular, and then dip N.W. On the west
they form the great mass of Ben Bhrackie; and from their southern
slopes we have, at Clunie, the limestone band of Pitlochrie again
making its appearance.

This parallel of Limestone, which has a N.W. dip, and which I
regard as a continuation of that seen on the north side of Loch Tay,
extends itself still further eastwards; it has been worked at the
Market Muir, about half a mile N. of the village of Kirkmichael. It
is now wrought two miles K. of Kirkmichael, at Dunien, where it is

264 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

well seen, dipping N.N.W. at 35°, and is of a uniform light-grey
colour, with very distinct bedding and lamine, and possessing litho-
logical features which very nearly ally it to some of the carboni-
ferous limestones. No traces of fossils, however, occur init. At
Dunien, on its south side, trap appears. From Dunien eastwards
its course is well seen. It has been quarried at Balchraggan and
Soilairzie (at the latter place it has white lenticular bands of pure
carbonate of lime along the lamin); and from hence it extends
across Glen Shee by Mount Blair into Glen Isla.

With reference to Glen Shee, the valley being open and the
country on the hill-sides to a great extent clothed with heath, the
sections are not so satisfactory as in many other portions of the
Highlands. A dark-grey limestone was, however, formerly worked
at Balanzien, about two miles 8. of the Spittal. The exposure here
is only imperfect, and the limestone apparently dips N.(?) On the
hill on the north side, a fine-grained grey syenite is seen. From
the Spittal, up Glen Beg, on the north side, great masses of red
porphyry manifest themselves; but the same grey limestone of Bal-
anzien becomes again visible in the higher part of Glen Beg; and,
from the verdant herbage on the S. side of the stream, this limestone
would appear well developed in this valley. At the spot on the
road-side where it has been wrought, its arrangement is irregular
and its dip indistinct. In the hill above this quarry on the N., con-
torted gneiss is seen with a N. inclination. From the section here
no definite conclusions can be arrived at concerning the relative
arrangement of the gneissose limestones and quartz-rocks. The
influence of the plutonic area, which commences on the 8.W. of the
Ben-y-Gloe Mountains, and, extending eastward, unites with the
great granitic areas of Aberdeenshire, has so far broken up the several
metamorphic rocks as to render their arrangement almost unintelli-
gible in the regions which he immediately south of this plutonic
area. With reference to Glen Tilt, Macculloch alludes to the confused
arrangement which prevails in this valley among the strata. There
are, however, certain statements occurring in his memoir (Geol.
Trans. vol. iii.) which lead to the inference that on the south side of
the Tilt the limestones “‘ invariably” dip to the south at varying
angles (p. 305); and as regards the quartz-rocks of Ben-y-Gloe,
Macculloch remarks that these are seen alternating with limestones,
which are again succeeded by the mica-slate (p. 307). The follow-
ing statement also occurs :—‘‘ We have seen that the great mass of
quartz-rock is followed by a small bed of limestone, and that this
again is succeeded by micaceous and clay-slate, terminating the
series of the bedded rocks in this direction” (alluding to the south)

~oty).
ee the sections which have already been described, and from
the observations of Macculloch, it is evident that the sequence of
rocks from the margin of the quartz-rock area towards the southern
limits of the Grampians is as follows :—First and lowest, quartz-
rocks ; secondly, grey limestones, in some instances with lenticular
bands of white carbonate of ime. These lmestones are of very

y=

1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. 265

varying thickness, and in some instances appear to thin out alto-
gether; and are succeeded by, thirdly, the gneissose rocks, which
occupy so great an area in the Highlands of Scotland.

: J § 7. Sections N. W. of the Great Zone of Quartz-
rocks and Lamestones. Section from Glen Lyon
to Loch Treig (fig. 6).—Allusion has already
been made to the black gneiss which is seen
having a 8.E. dip in the north side of the quartz-
rock zone at Inverwick. In Glen Lyon, rocks of
this nature, and with only slight modifications in
their dip, extend themselves to the western end
of Loch Rannoch, where an extensively deve-
loped area of syenite occurs; and from this syenite
% the gneissose rocks usually incline south-eastward
in the neighbourhood of this lake.

The area occupied by this syenite, as shown in
geological maps, fails to afford anything like an
adequate idea concerning the extent of country
which this rock covers. From the head of Loch
Rannoch it extends along the mountain-road lead-
ing to Fort Wiliam—at least as far as Loch Ou-
chan, and from this, westward, almost to Loch
Treig; but its area was not definitely determined.
In the form of a flesh-coloured porphyry, this
plutonic rock occurs in all the streams which
drain the hills lying N. and §. of Oise-dhu, and
the lakes through which this stream flows in its
course to the Leven. This great plutonic area,
coloured as gneiss in geological maps, seems to
abut against the trap-rocks of Glen Coe.

At the head of Loch Treig we find it flanked by
eneiss, which dips N.W., or from its 8. margin,
as at Loch Rannoch; the same rock inclines S.E.
from its southern boundary.

§ 8. Section from King’s House, through Glen
Ove, to Ballahulish (fig. 7).—The plutonic rocks
just referred to extend to King’s House; but on
passing westwards towards Glen Coe, the dark
porphyries and trap-rocks which exclusively fill
this gorge, soon make their appearance. They
occupy the whole of the glen to Claichig, where
we have stratified rocks coming abruptly against
the traps, as seen on the hill-slope immediately
opposite the small inn at Claichig.

These stratified rocks dip W.N.W. at 45°, and
they have somewhat of a gneissose aspect, but are
much more highly siliceous than ordinary gneiss.
Maccullochalludestotheirdiftering from mica-slate,
and designates them schistose ‘“ quartz-rocks*.”

* Geol. Trans. vol. i. p. 475.

Gneiss.

wd F

Fad =a Fath
CLS Aa AY,

Syenite and Porphyry.

Fig. 6.—Section from Glen Lyon to Loch Treig. Distance 20 miles.

Glen Lyon.
Quartz-rock.

S.E.

266 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

They vary altogether from the rocks which occur to the west of
them; and from their nature and position I look upon them as the
representatives of the true quartz-rocks. At Ballahulish they are

Fig. 7.—Section from Glen Coe to Ballahulish. Distance 8 miles.

E.S.E. ns W.N.W,
Glen Coe. Claichig. Ballahulish,

Tv

oe
TI CR NN
: 5 NE 4A CWS
Nie 4y~= yan a7 Tp( 40% Loe a’ = TIN
Se ASAIN OS ES EP SANG . SSK SS
Porph and Trap-rock. Quartz-rock. Limestone: Schist.

y Pp

succeeded by the dark-grey limestone, above which occurs the slate
of this locality, having the same direction of inclination—viz.
W.N.W.

§ 9. Section across the Peninsula of Ardsheal from Benivair (fig. 8).
—Immediately E. of the inn at Ballahulish syenite again makes its
appearance, and this mass of syenite extends 8.W. along the coast
to near Ardsheal, where it becomes flanked on the coast by meta-

Fig. 8.—Section of the Ardsheal Peninsula. Distance 3 miles.
: w.

Benivair. Lhinne Loch.

I

E

1
'
1
‘
‘
1
1
‘
1
1
‘
1
1
t
i

d. Schist. c¢. Limestone. a. Quartz-rock. * Syenite and trap-rocks.

morphic rocks, in the form of quartz-rocks and lmestone. On the
east of the Ardsheal peninsula the syenite is seen forming the hill of
Benivair, against which, on the west, there occurs a mass of quartz-
rocks, which, when in proximity to the syenite, contains crystals of
felspar, and becomes almost a porphyry. This quartz-rock, more
remote from the syenite, is much intersected by joints, and has the
stratification very indistinct ; but the lamine incline at a very high
angle, N.W. This quartz-rock at Ardsheal is worked for ceramic pur-
poses, and is know nunder the name of “ china-rock.” On its N.W.
side it becomes more distinct in its stratification, and is succeeded by
a grey limestone, about twelve feet in thickness. Above this lme-
stone the dark-grey slates are seen dipping in the same direction ;
but on passing over the Ardsheal peninsula, the inclination of these
slates becomes reversed. On the western side the quartz-rocks
again make their appearance, dipping under the slates; and these
quartz-rocks repose against another mass of syenite, which forms
the extreme west of the Ardsheal peninsula. In the west portion
of this section no limestone is seen ; and this may either result from
the thinning out of the narrow limestone-band, or the limestone may
exist, but not be visible, from the covering up of the junctions by soil.

The south-east side of the Ardsheal section exhibits the arrange-

1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. 267

ment of the rocks seen between this locality and Appin. At Port
Appin thick masses of quartz-rocks are seen, which are greatly con-
torted, having a prevailing 8.E. dip. These are succeeded con-
formably by dark slates; and the arrangement here represents the
N.W. end of the Ardsheal section.

The limestone islands which occur in Loch Linnhe exhibit cal-
careous strata in great development. In Sheep’s Island these lime-
stones are much contorted, and very nearly perpendicular, but with
a predominant 8.E. dip. Judging from this, we might be induced to
infer that the strata here pass under the quartz-rocks of Port Appin ;
and if this be the case, they represent a zone of calcareous rocks
altogether different from that previously alluded to, and, under such
circumstances, they must be regarded as the equivalents of the thick
limestones of Assynt. But perhaps it may be premature to arrive at
this conclusion without more evidence than that at present afforded
by the sections on this coast.

The sections which the districts lying N.W. of the area of quartz-
rocks and limestones already referred to exhibit show, with probably
the exception of the islands in Loch Linnhe, a sequence of stratified
deposits very nearly allied to that which the region 8. of this zone
manifests. Quartz-rocks at the base, succeeded conformably by
limestones, and these by gneissose or dark slaty rocks, make up the
stratified beds N.W. of the zone of “ quartz-rocks and limestones ”
which extend from Jura to the N.E. coast of Scotland. The rocks
in the areas separated by this zone represent each other in arrange-
ment and almost in mineral nature,—the only difference being in the
character of the highest member, which occurs as a blackish slate
on the west coast, while towards the south-east its equivalent has a
gneissose aspect. This conclusion, as to similarity in age and position
among the deposits south of the Caledonian Canal, supposes the ex-
istence of a great line of fault traversing the Grampians in a 8.W.
and N.EK. direction; and this line of fault—parallel to the great
S.W. and N.E. fault along the southern margin of this range of
mountains separating the metamorphic rocks on the N.W. from the
Old Red Sandstone series on the 8.E., extending from sea to sea—is
well seen in Glen Lyon along the northern edge of the quartz-rocks.
On the N. of this line of fault we have a great downthrow, the
higher beds of the series (the gneissose rocks) being again repeated ;
and as we approach the N.W. coast of Argyllshire, we have the
lower members (the limestones and quartz-rock) again brought to
the surface by the agency of plutonic masses.

With reference to the relations which these quartz-rocks, lime-
stones, and gneissose strata, constituting so much of the great mass
of the Grampians, bear to other rocks of a similar nature in the
N.W. and N. of Scotland, I cannot better illustrate this than by
referring to Sir Roderick Murchison’s “ Section across Lochs Eriboll
and Hope*.” In this section the upper quartz-rocks, upper lime-
stone, micaceous and quartzose flagstones, and micaceous and gneissose
flagstones represent the series of strata which form the Grampians 8.

* Quart. Joura, Geol. Soe., vol. xvi. p. 226.

268

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Feb. 20,

of the Caledonian Canal, as exhibited in the sections; and the results
of my observations have induced me to conclude that on the main-
land the lower rocks of this section are not represented, and that we

Distance 20 miles.

Mig. 9.—Section from Malin Head to Inishowen.

Malin Head.

tod
=)
Sf
as
=
oX
ay
Ss
a)
-= 9
J
&
oO

* Syenite and Trap-dykes.

a. Quartz-rock.

Limestone.

C.

Gneiss.

d*,

Chlorite-schist.

d.

have no metamorphic rock, either in na-
ture or arrangement, in this great area of
Scotland, that can be paralleled with the
“fundamental gneiss” of Sutherland and
Ross.

§ 10. The Arrangement of the Metamor-
phic Rocks of the County of Donegal, and
Section of the East Side of Lough Foyle
(fig. 9).—On that portion of the Irish
coast which is most nearly contiguous to
the south-western extension of the quartz-
rocks and limestones of the Grampians, we
have a great development of rocks of a me-
tamorphic character. Almost the whole of
the County of Donegal is made up of rocks
which appertain to this series ; and with
them are associated plutonic masses. Of
the deposits in this area the greater por-
tion consists of gneissose strata, nearly
allied in lithology to the chloritie schists
of the 8.W. parts of the Grampians.

These chloritic schists, which in geolo-
gical maps of Ireland are generally termed
mica-slates, are subjected to great flexures.
They have prevailing N.E.-S.W. strikes ;
and, on the whole, 8.E. dips are predo-
minant. Like rocks of a similar nature,
these gneissose rocks of the North of Ire-
land manifest themselves under such cir-
cumstances as to induce the conclusion that
they occupy the higher zone amongst the
deposits of this region. Beneath these
eneissose rocks of Donegal there is seen a
thick series of quartz-rocks, having the
same strike, and being subject to the same
flexures and dips as the overlying strata.
In many localities in the North of Ireland,
between the quartz-rocks below and the
eneissose strata above, there occurs a dark-
grey limestone ; and in some areas, where
the flexures become flattened, this lime-
stone covers a considerable surface. This
limestone, which is well seen at Culdaff,
on the N.E. side of the Inishowen penin-
sula, occurs in other localities between the
quartz-rocks and the gneissose beds, but.
has hitherto yielded no fossils.

1861. ] HARKNESS—HIGHLANDS AND N. IRELAND. - 269

In this arrangement of the metamorphic deposits of Donegal we
have an exact counterpart of the Highland series; and this affinity
becomes still more apparent when we examine in detail the section
afforded by the N.E. coast of this country from Inishowen Head to
Malin Head, the extreme North of Ireland (fig. 9).

Commencing at the S.E. end of this section, we have exhibited
the usual chloritic schists of the North of Ireland with the prevailing
8.E. dips, frequently the result of reversed flexures, which are nu-
merous in this district. This chloritic schist forms the Mountain
of Craignamaddy. Rocks of this nature extend north-westward to
the neighbourhood of Tramore Bay, where the quartz-rocks begin to
show themselves, having the usual 8.E. inclination. These quartz-
rocks occupy the coast between Tramore Bay and Dunmore Head ;
and at the latter spot the chloritic schists again make their appear-
ance, the result of an anticlinal curve in the quartz-rocks, pushing
over the latter towards the N.W., and bringing in the small patch of
schist which forms Dunmore Head.

Immediately north of Dunmore Head the limestones, dipping
under the chloritic schists, occur. These limestones of Culdaff are
not seen on the shore, owing to the district being low and covered
with sand. Ata short distance inland they are very apparent, and
marked by flexures, which spread the beds over a considerable area.
The limestones here possess the prevalent 8.E. dips.

North of Culdaff large masses of trap are seen extending onwards in
a W.S.W. direction, to beyond the village of Malin. On the line
of the section N. of these traps, another exhibition of quartz-rocks
occurs, intersected by other traps; and this area of quartz-rocks
extends for more than two miles, after which chloritic schists again
make their appearance. This second mass of quartz-rocks with the
prevailing S.E. inclination has had its origin from the same circum-
stances which gave rise to the area south of Dunmore Head, viz.
from an anticlinal pushed over towards the north. These two areas
of quartz-rocks, separated from each other by the chloritic schists of
Dunmore Head, are seen in the district south-west of Cardonagh, and
they form the quartzitic area which is well developed on the east
side of Lough Swilly ; from whence they extend south-westward to
Lough Muck, and terminate in a point flanked on the N.W. by the
granite of the Derryveagh Mountains, and on the 8.E. by the great
area of gneissose rocks.

Continuing the section north-westwards, the chloritic rocks suc-
ceeding the quartz series are well seen at Glengad Head. They
also form the Mountain of Maheryard, and possess, as regards dip and
arrangement, like features to those of the masses of these rocks
which occupy the more southern area. A little to the north of Maher-
yard the quartz-rocks again appear, supporting the chloritic schists,
and have a continuous 8.E. dip from the junction with the chloritic
rocks to a spot called Sandy Port.

This latter surface of quartz-rock is much intersected by traps ;
and at Sandy Port a well-marked axis is seen, from which reversed
dips occur. Near this axis the quartz-rocks put on an aspect dif-

270 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Feb. 20,

ferent from that which they generally assume. They have a pink
colour, are much broken up, are devoid of regular arrangement, and
exhibit features nearly akin to hornstone. At Sandy Port, traps are
seen ; but these have not produced the results above alluded to, and
such results do not accompany the other outbursts of trap, which are
so abundant along this coast.

These changes in the quartz-rocks have originated from plutonic
masses; and although rocks of this character are not seen imme-
diately on the north-east coast of Donegal, yet at a short distance
inland such rocks occur.

The rock which has produced the hornstone aspect in the quartz-
rocks, and given rise to this well-marked axis, is a red syenite, very
manifest on the west side of Malin Head; and this red syenite
occupies a considerable area in the north-west of the county of
Donegal.

From this axis at Sandy Port the quartz-rocks continue north-
westward to Ballyhillin, where they are succeeded by the overly-
ing gneissose series.

On the north side of this axis the higher members, which south-
ward consist of chloritic schist, are represented by a flaggy gneiss,
which is well seen in the precipitous rocks on the north-east side
of Malin Head ; and lithologically this gneiss is very much allied to
the: upper gneiss of Sutherland. Traps are very abundant among the
rocks which form the north-east extremity of Malin Head ; and thick
veins of white quartz are also prevalent in this locality.

With reference to the West of Ireland, where rocks consisting of
eneiss, limestone, and quartz-rocks are shown to occur, I have not
had an opportunity of comparing these as they are exhibited in the
County of Mayo with the North of Ireland and with the Highland
rocks. But, inferrmg from the strike and the arrangement of these
rocks as they are laid down on the geological map of Ireland, I feel
little doubt that they are referable to the same position and sequence
as the rocks of a similar nature in the North of Ireland and in the
Highlands of Scotland, and that the true position of these rocks is that
assigned to them by Sir Roderick Murchison in his “ Hypothetical
View respecting the Gneissose Rocks of the Southern Highlands”
(Quart. Journ. Geol. Soc., vol. xvi. page 238).

P.S. [April 6th. |—Since the above memoir was read, the author has
again visited the limestone which is worked at Leny, near Callender,
for the purpose of endeavouring to procure fossils from the associated
black shales. After a careful and diligent search, no specimens could
be detected, although the limestone is now being wrought to a con-
siderable extent. The face at present exposed shows a greater
extent of rock than that above referred to,—no less than twelve feet of
limestone with thin black shales being visible, and having well-de-
veloped black shales both above and below. A dyke of porphyritic
felstone, which cuts the limestone very obliquely to the west of the
quarry, is also seen on the north side of the limestone.

1861.] DREW—HASTINGS SAND. 271

Although no fossils were seen, the phenomena of cleavage, which
are by no means well developed among the rocks constituting the
Grampians, are beautifully shown in the shales associated with the
limestone in this spot. These possess a cleaved structure to a great
extent, having, in some instances, lost all traces of their original
bedding. The thin limestones, however, are devoid of this structure,
—a circumstance which supports the inference that, although the
rocks of the Grampians have been subjected to the pressure which
results from great flexures and contortions, the lithological nature
of the strata was such, except in the case of the shale-beds, that no
rearrangement of particles could take place to give rise to cleavage-
planes.

Marcu 6, 1861.

Francis George Shirecliff Parker, Lieut. H.M. 54th Regiment,
Roorkee ; and J. Gwyn Jeffreys, Esq., 25 Devonshire Place, Port-
land Place, were elected Fellows.

The following communications were read :—

1. On the Successton of Brps in the “ Hastinas Sanp” wm the
Nortuern Portion of the WEALDEN AREA. By Freperic Drew,
Esq., F.G.S., of the Geological Survey of Great Britain.

ConTENTS:

I. Introduction.
II. Wealden Formations in the Meridian and Neighbourhood of Tunbridge

Wells.
1. Weald Clay. 3. Wadhurst Clay.
2. Tunbridge Wells Sand. 4, Ashdown Sand.

A. Presence of the Ashdown Sand in the Railway-cutting between Tun-
bridge and Tunbridge Wells, and the Extent of the Tunbridge Wells
Sand to the Northward.
III. Eastward of the Meridian of Tunbridge Wells.

1. Weald Clay. 4, Ashdown Sand.
2. Tunbridge Wells Sand. 5. Hastings Sand around Hastings
3. Wadhurst Clay. and Battle.
IV. Westward of the Meridian of Tunbridge Wells.
1. Weald Clay. 2. Tunbridge Wells Sand. Upper

and Lower, with the intermediate ‘‘ Grinstead Clay.”
VY. Nomenclature of the Hastings Sands.
1. Dr. Mantell’s Nomenclature.
2. Reasons for using the Names now proposed.
VI. Weald Clay of the Neighbourhood of Horsham.
VII. Conclusion. Lithological Characters of the Hastings Sand.

I. Introduction.—Having for the last two years been engaged (in
the course of the progress of the Government Survey) in examining
part of that large tract in the south-east of England which is made
by the outcrop of the Wealden strata, and having now become ac-
| VOL. XVII.—PART I. t

272 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

quainted with many details concerning that formation, I wish to
bring before the Society an account of its lithological character and
of the order of succession that prevails in it.

As regards this part of England, the Wealden formation has long
been divided into three members, namely—

The “‘ Weald Clay,’’ the “‘ Hastings Sand,” and the “ Ashburnham
Beds.”

The first, the ‘‘ Weald Clay,” is much the same through all its
thickness ; where there is variety in it, it has been well described by
Dr. Fitton, Mr. Martin, and Dr. Mantell. The lowest member, the
“« Ashburnham Beds,” which may, perhaps, be classed with the Pur-
beck formation, does not appear in that district in which I have more
particularly been engaged. I shall therefore say little of these two,
and almost confine myself to the ‘ Hastings Sand,” and to the north-
ern part of the Hastings Sand country, a district, 50 miles long and
varying from 3 to 12 or more in width, lying between and in the
neighbourhood of the towns of Tenterden, Cranbrook, Tunbridge
Wells, East Grinstead, and Horsham.

This ‘‘ Hastings Sand,” it is well known, has much clay and a
little of other substances interstratified with it; and something has
been done towards finding out the order and character of its divi-
sions, especially in certain districts; but these are small in extent
and are separated from one another, no good comparison of the beds
in each has been made, and some of the accounts given seem to be con-
tradicted by the facts which I have lately observed. I therefore think
it well to lay these before you, with my notions as to their bearing
on what was before known ; and I believe they will do a good deal
towards connecting together the various information you are already
in possession of, and clearing up some points on which doubt or con-
fusion has been felt.

It will be best first to repeat as shortly as possible the conclu-
sions arrived at by those who have written about these strata.

Dr. Mantell, who had paid more attention than any one else to the
Wealden formation, and who was particularly successful in the dis-
covery and the study of its organic remains, gives the following as
the succession of beds :—

Weald Clay, stiff brown and blue clay; then the Hastings Sand,
divided into—

1. Horsted Sand: light-coloured sand and sandstone.

2. Tilgate Beds: sand and sandstone, gritstone (calcareous sand-
stone), and clay or shale.

3. Worth Sands: white and yellow sand and sandstone.

The name of No. 1 is taken from a place, which I have not visited,
not far from Lewes; No. 2 is called “Tilgate Beds” from Tilgate
Forest, some miles east of Horsham; No. 3 is named from its occur-
rence, according to Mantell, at Worth, near Crawley. In the neigh-
bourhood of Hastings, where the best sections are to be seen, Dr.
Mantell recognizes the same series of strata as he observed in the
more western parts whence he took their names; and he describes

1861.] DREW—HASTINGS SAND. 273

Horsted, Tilgate, and Worth Beds as having just the same characters
in the two districts.

Dr. Fitton, in his valuable paper on the strata below the chalk,
gives some detailed sections of what was to be seen on the face of
the cliffs west of Hastings ; and these have come to be the more im-
portant from much of what was then visible being now obscured by
the buildings of the town of St. Leonards. Dr. Fitton did not at
that time connect what he observed into a system of strata; but
subsequently, in a “ Sketch of the Geology of Hastings,” written by
him, he adopted provisionally the same division as Mantell did.

The information given in the older books and papers may be con-
sidered as merged in these conclusions of Dr. Mantell and Dr. Fit-
ton: so I need not speak further of them ; for I do not wish to give
here a history, but an account of the latest and best state of the
knowledge of this formation. More lately, however, than all this,
Mr. Morris and Mr. Prestwich described to the Society* the cuttings
that were being made for the Tunbridge Wells Railway; and, though
they were not quite sure that they understood the succession of the
beds exposed in them, they gave their idea of what it might be. As
the part examined by them is included in that which I intend to
speak of somewhat minutely, I will leave the discussion of their views
for the present, and pass on to my own description of the rocks.

In giving this, I will first speak of them as they occur in the
neighbourhood of Tunbridge Wells—for many reasons a convenient
part to begin with; I will then give a short account of what they
are on the east of that place ; and lastly, we will trace them in the
other direction as far westward as where the Hastings Sand dips
beneath the Weald Clay.

II. In the Meridian and Neighbourhood of Tunbridge Wells.

1. Weald Clay.—In the meridian of Tunbridge Wells I find the
Weald Clay to consist nearly all of clay and shale of different colours,
blue, brown, yellow, &c. It has one or two thin bands of Paludina-
limestone, and some calcareous grit and clay-ironstone ; the thick-
ness I believe, from what I hear of borings into it at Maidstone, and
from what I see of the fall of ground between where its upper beds
occur and the outcrop of its base, to be not less than 600 feet +.

* Quart. Journ. Geol. Soc., vol. ii. p. 397. 1846.

+ The following are the crounds for this estimate. A boring at Brenchley: 8
Brewery, at the bottom of Gabriel’s Hill, Maidstone, which began about at the
top of the Weald Clay, went through 500 ft. of clay (passing a water-bearing
sand at 100ft.), and did not reach the bottom. Another boring, at Allnutt’s
Paper-mill, Tovil, near Maidstone, began at the top of the Weald Clay, passed
a water- -bearing sand at 115 ft., and went through, on the whole, 600 ft. of clay
down to a hard rock, which they did not pierce, and which very likely was the
top of the Hastings Sand. Again, the top of tie Weald Clay at River Hill, on
the Greensand escarpment, is 500 ft. above the sea-level ; at Leigh (which bears
from River Hill in a direction at right angles to the strike of the beds) the base
of it is 80 ft. above the sea-level. Therefore, if the beds were flat between those
two places, there would be a thickness of 420 ft.; but it is very likely that there

v2

274 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

The boundary between it and the first stratum of the Hastings Sand
is sharply defined: in many places, as at the river-bank below Ram-
hurst Farm near Tunbridge, at Capel on the east of that town, and
at Culverden Quarry and Rusthall Common, both near Tunbridge
Wells, the clay is seen to rest immediately on good sand or sandstone.
At a certain height, however—perhaps thirty feet—above the junc-
tion there is a layer of loam with a little sandstone, which may vary
from twenty to a very few feet in thickness. This is within what I call
“Weald Clay.” Between this layer and the stratum-level that I
take for the boundary, is stiff clay or shale, sometimes containing
lenses of calcareous grit *.

2. Tunbridge Wells Sand.—The first layer of the Hastings Sand
IT call “ Tunbridge Wells Sand”; and in using this and other names
of my adoption I have been guided by reasons which will best be
given towards the end of this paper.

The top of the Tunbridge Wells Sand is hardly seen on the first
outcrop of it from beneath the Weald Clay, though at these points—
namely, on the left bank of the Medway on the west, and by Sandlin
and Capel-bank on the east of Tunbridge—there are moderately good
sections; but it is well shown in several parts of that great spread
of this subdivision which occurs all around Tunbridge Wells. The
top bed is in many places a fine, hard, white sand, with few or no
partings or distinction of beds in it, similar in composition to that
thick bed of sand underneath the Castle and in the Kast Cliff at
Hastings, though this belongs to another horizon. It is stuff that is
difficult to work out, and sometimes requires even blasting; but
when separated into fragments, a touch will break it into loose sand.
In other places the bed is a soft, generally buff-coloured, or else
light-brown building-stone in a massive bed. The gradual change
from the first kind of substance (which may conveniently be called
‘“‘rock-sand’’) to the other is well seen along two or three different
lines—namely, from Tunbridge Wells by Rusthall Common to Lang-
tont, from the High Rocks to the summit of Groombridge Hill, and
from Eridge Rocks to Alksford and Sherlock’s. I have measured at
different places 25, 35, and even 48 feet of the rock-sand, and of the
equivalent bed when sandstone 10, 12, or 16 feet, generally in one
thick, pretty hard layer. Beneath this well-marked top bed come
still sandy beds, but not massive ones like the first; for the greater
part of the Tunbridge Wells Sand may be described as soft, buff or
light-brown sandstone in beds of half a foot, 1, 2, 3, or more feet
thick, interstratified with beds of loam, thin beds of clay, and now
and then some rather loose sand. The whole thickness of the subdivi-
sion seems to be 160 or 180 feet. I judge it to be as much as this
is a general dip to the north (in one or two places I have seen the beds dipping
in that direction) ; if it were only half or three-quarters of a degree, the thickness
would be 600 feet. I am indebted to Mr. Bensted, of Maidstone, for the infor-
mation about the borings.

* Tn the following localities :—River-bank nearly a mile east of Leigh; rail-

way-cutting north of Penshurst Park ; near Fordcombe, &c.
t Marked Lengthington Green on the Ordnance Map.

~

1861. ] DREW—HASIINGS SAND. 275

at Tunbridge Wells, from the great descent there is between the out-
lier of Weald Clay at the top of the Common, by the corner of Bishops-
down, and the valley of the Wells; and even in this the base of the
sand is not reached, while the dip is in that direction which would
make out the thickness more than the fall of the ground. At Groom-
bridge Hill too, where the strata are about flat, there is 180 feet of
vertical height from the top to the bottom of the sand. At Eridge
Rocks, however, and at some other places, there can hardly be so
great a thickness.

I should here mention those natural sections so well known to
every one who has been in the neighbourhood of Tunbridge Wells:
they are lines of projecting rock sometimes showing a quite perpen-
dicular face. From their having a grey weathered surface, and from:
the way in which the vegetation is combined with them, clothing
and hanging over the summits, they form, in several places, exceed-
ingly pretty groups. All of these (namely those on Tunbridge Wells
and Rusthall Commons, Eridge Rocks, Harrison’s, Penn’s Rocks, &e.
belong to one stratum, namely the top bed of the sands that I have
before described; and it is to be remarked that these bare rocks
occur where the bed is not in its hardest form (namely a good
sandstone), but they are almost in every case composed of rock-sand,
which would seem to resist the degrading action of the weather by
the solid mass it presents without planes of division. It will gene-
rally be found that the rocks are capped with an outlier of clay, which
is of course the Weald Clay. There is one more circumstance about
the Tunbridge Wells Sand which I would have borne in mind, be-
cause it bears on a question we shall come to discuss; it is that some-
times at a level quite low down in this subdivision another bed of
rock-sand occurs; it does not, however, form any natural rocks. It
may be seen by Groombridge, Speldhurst, Nashes near Penshurst,
and at other places.

3. Wadhurst Clay.—We now come down to a clay stratum, which
I call “ Wadhurst Clay.” The bottom of the sand is generally loamy,
this being the passage (not a very gradual one) to the clay that suc-
ceeds. This last is, both in the upper part and through all its thick-
ness, stiff brown clay, or brown or blue shale; it ends sharply against.
the next sandy stratum, good clay or else shale resting on sand or
sandstone. The thickness was proved by a well-sinking at Pellet
Gate, Pembury, to be 160 feet; but I do not think it is everywhere
quite so much; I should say that in the neighbourhood of Tunbridge
Wells it varied between that and 120 feet. There occurs a little of
three different kinds of stone in this clay,—first, a calcareous grit,
or a fine, hard, calcareous sandstone, which is seen in thin beds every
here and there; but just in the neighbourhood of Beech Green,
Withyham, it forms beds of two or three feet, much worked for
roadstone. Secondly, a shelly limestone, containing Cyvena chiefly,
of which I only saw a few two- or three-inch layers. Thirdly, a
smooth grey clay-ironstone, generally in small nodules or layers
of nodules. It was this kind of ironstone, and chiefly stone from

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276

1861.] DRHW—HASTINGS SAND. 277

this very stratum, that was dug to supply the furnaces that once
abounded in this part of the country. The shallow round pits by
which it was extracted can yet be seen in many of the woods ; they
must not be confounded with the large openings, now partly filled
up and much overgrown, or else forming ponds, that were made,
also many years back, to get shale, or “ marl” as they call it
here, with which it was the custom to dress the land. It may be
that im digging this out they put aside and carried to the furnace
whatever ironstone was met with: all tradition, however, points to
the small shallow holes as the source of the ore, which went (and
still goes) by the name of “‘iron-mine” or ‘‘mine-stone,” while the pits
are called ‘“mine-pits,” and the large places are everywhere recog-
nized as “‘marl-pits.” I should mention that on the south of Wad-.
hurst Tunnel, in the railway-cutting, I saw a thickness of 15 feet of
sandstone and loam in this clay, and once or twice besides I have
seen traces of a similar bed. It is likely enough that the same sort
of thing occurs in other places, where it escapes notice (for in a clay
country deep sections are always scarce); yet I have seen enough
to be convinced that this bed is very nearly all of clay.

4, Ashdown Sand.—The “‘ Ashdown Sand” comes next; it has no
character to distinguish it from the Tunbridge Wells Sand; the
two can only be separated by regarding their positions with respect
to the Wadhurst Clay, or, if this fails on account of faults being
present, by sight and quite local differences. It is a similar collec-
tion of layers of sandstone and loam with an occasional bed of rock-
sand; and it has this further resemblance, that the top is Im many
places a good thick bed of rock-sand: this is well seen in four or
five of the valleys lying on the north of the road from Wadhurst to
Mark Cross, which reach through the clay to the Ashdown Sand. I
do not think I have found this bed making natural rocks like the one
at the top of the other sands.

Clay-ironstone occurs occasionally in the upper sandy subdivision;
but yet more is found in the Ashdown Sand. A good deal may be
seen in the heaps brought up from the Wadhurst Tunnel and thrown
out above it; and in the railway-cutting, a mile and a half further
down the line, it has lately been worked to see if it would answer to
transport it to the North. On Ashdown Forest, too, it occurs fre-
quently, generally with a coating of brown iron-ore; there are two
or three pits where it is now being dug for roadstone; and I have
heard that about here like stone used to be extracted from the sand
for smelting.

A bed of clay and shale occurs in these sands; it is seen at several
points south of Frant and along the north of Ashdown Forest; at
the latter part it appears to be 30 feet or more in thickness.

These sands have a great spread about Ashdown Forest ; it is in-
deed the central district of the Hastings Sand, where these low beds
rise and make the highest ground of any in the whole formation.

The deep valleys that cut across Ashdown Forest reach down to
such a depth as to expose, I should think, 250 feet in thickness of

278 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

the sands, without reaching to their base; for the lowest beds seen
(those at Crowborough Mills seem to be so) are of just the same
sort of sandstone and loam. Some miles north and north-east of this
there are other tracts of this sand, of very irregular forms; they are
brought to the surface by one or more anticlinals that run somewhat
east and west. There are two inliers* of it quite near to the
country of the Weald Clay itself; namely, one a few miles to the
south-east of Edenbridge, and another that stretches from Penshurst
to beyond the line of railway between Tunbridge and Tunbridge
Wells.

A. Presence of the Ashdown Sand in the Railway-section from
Tunbridge to Tunbridge Wells, and the Extent of the Tunbridge Wells
Sand to the northward.—It is just at this part that the beds were
examined by Mr. Morris and Mr. Prestwich, whose description of
them is printed in the Society’s Journalt. In making a comparison
of this with the results of my own observations, I must refer you
to the transverse section, fig. 2, p. 276. Mr. Morris and Mr.
Prestwich began their observations by the Tunbridge Tunnel; and
just on the south of it they saw sandstone beds coming from under-
neath a great thickness of clay and shale. Passing on through seve-
ral cuttings, and rightly interpreting a fault (the throw of which,
however, they somewhat overrated), they came to shale again, this
time overlain by sandstone. This, however, they take to be a lower
bed of shale (partly from its differmg from the other in being unfos-
siliferous), and they consider this sandstone, which continues on to
Tunbridge Wells, to be in the same part of the series with that they
first saw, accounting for the position of the shale by supposing a
second fault, concealed in the valley. I am, however, convinced
(and I have no doubt that Mr. Prestwich and Mr. Morris would have
come to the same conclusion if they had been able to extend their
observations for a few miles to the east and west of the railway) that
these last shales, coming from underneath the Tunbridge Wells Sand,
are the upper part of the bed of which the shales at the Powder-mill
and Tunbridge cuttings are the lower (namely the Wadhurst Clay),
and that the sandstone underneath them at the latter places is the top
of the Ashdown Sand. This I have proved by tracing the shale around
this inlier of sand which I observe to come from underneath it ; while
the shale, in its turn, is covered by the mass of sand from Bidborough
to Tunbridge Wells, as well as by like sand on the other side of the
valley, and is capped by two or three outliers of sand nearer to Tun-
bridge. The difficulty in the way of this explanation, which they

* T doubt if this word 7zz/zer is enough in use to be allowed to pass without
explanation ; for I have never seen it in print. It meansa space occupied by one
formation which is completely surrounded by another that rests upon it. It is
useful to have a word that will express this ; and “inlier”’ is a very appropriate
one; for the circumstance to be named is the exact converse of “ outlier,’ which
is an isolated mass surrounded by a formation that underlies it; and the advan-
tages of “inlier”’ are manifest over such a phrase as was used in the same sense

by the late Mr. P. J. Martin, namely, “outlier by protrusion.”
t+ Quart. Journ. Geol. Soc., No. 8, vol. ii. p. 397.

1861.] DREW—HASTINGS SAND. 279

rejected on that account, is that there are few signs of such a thick-
ness of sand as that of all the Tunbridge Wells beds on the north of
the Tunbridge Tunnel; I have, however, seen sand resting on the
clay close there, and not far off are one or two sections showing no
inconsiderable thickness of it. The greater part of the space between
that and the Weald Clay is flattish ground, covered either by a loamy
alluvium or by gravel; and, of course, sections through this are
scarce; but I have seen some sand as far away as a quarter of a mile
to the N.W. of Tunbridge Town. The Tunbridge Wells Sand, then,
must have its first outcrop along here, though there is no great feature
of ground such as one would expect ; for along this part, where there
is a special line of elevation, the ground has been denuded to quite
a low level.

Ill. Eastward of the Meridian of Tunbridge Wells.

1. Weald Clay.—The foregoing, then, are the beds that are found
in the neighbourhood of Tunbridge Wells—using the word “ neigh-
bourhood”’ in a somewhat wide sense: we will now look at them in
the more easterly part of their outcrop (for I have traced them for
fifteen or twenty miles in that direction), taking them in the same
order as before. The outcrop of the lower part of the Weald Clay
is in flat ground, where there are few sections of any depth; and,
besides, it is hidden in many parts by some thickness of gravel; I
therefore cannot speak as to its exact character, but I find a pretty
well-marked line between the clay and the Tunbridge Wells Sand.
East of Tunbridge Town I quite lose sight of that loamy and sandy
bed which I said there was, on the other side, some forty feet up in
the clay.

2. Tunbridge Wells Sand.—The top of the Tunbridge Wells Sand
loses its rocky character a little before we get as far east as Brench-
ley, and becomes sandstone and loam not different from the rest of
the division, which itself is so much the same as I have before de-
scribed that I need hardly speak of it more. It may be mentioned,
however, that at a level that seems to be somewhat below the mid-
dle there is seen in some places a thin bed of clay and loamy clay,
partly red in colour, and underneath it a bed of rock-sand or else
thick-bedded sandstone. I cannot say for certain, but I think that
the clay-bed is not always present, but lies in patches, while the
rocky character of what is underneath it is more persistent. The two
beds can be traced as far east as the town of Tenterden. See fig. 1,
p- 276. Hardly any evidence could be obtained about the thickness
of the division; but it seems, from the space it occupies, to be much
the same as at Tunbridge Wells. .

3. The Wadhurst Clay.—The Wadhurst Clay is also like what it
is at Tunbridge Wells. I have but one thing new to remark on it:
the very top of it (the few feet below the junction with the sand) is,
in some places, especially near Cranbrook, of a rather red clay. The
thickness seems to be as much as 160 or 170 feet at Goudhurst, and
rather less in other places.

280 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

4, Ashdown Sand.—The Ashdown Sand, too, is the same as be-
fore. It still is rocky at or near the top; that is to say, thick-bedded
sandstone or rock-sand is found not many feet below the base of the
Wadhurst Clay; for the rest, it is such that one cannot distinguish
it from the Tunbridge Wells Sand. I have not seen any great thick-
ness of it. The bottom has not been reached.

_ 6. Hastings Sand around Hastings and Batile—These three beds,
then—two of sand with one of clay between them—spread over a
considerable area, without undergoing any great change; and beyond
this part, where I have myself examined them, Mr. Charles Gould,
who was then on the Geological Survey, made out at the same time
their succession about Hastings and Battle and further to the north-
west ; and he has described them in his notes in much the same terms
that I have used for them, though it would seem that the clay in
the middle (the Wadhurst Clay) is there of a less thickness, and has
a greater admixture of loam and sand, than in the more northerly
part. Mr. Gould and myself, though the districts we were upon
were quite separated, worked up to and identified a section in an
intermediate spot, so as to be sure of the true relation of the beds in
the two districts. Quite lately I have been in the very easterly
part, at Rye and thereabouts, and have found similar strata with the
same general character, and which may therefore be considered to
belong to all the Hastings Sand that is east of Tunbridge Wells.

IV. Westward of the Meridian of Tunbridge Wells.

1. Weald Clay.—Next in course we will follow the strata west-
ward from our first starting-point. The Weald Clay, as a whole,
continues the same. A sandy bed of no great thickness occurs near
the bottom, which appears to be a continuation of the one I men-
tioned before: it may be traced pretty distinctly as far as Ling-
field; and so may the horizon below it, which I fix on for the top of
the Hastings Sand; but west of Lingfield, for a length of about eight
miles, neither line is so definite. There is a good deal of loam in
the bottom part of the Weald Clay, and what clay there is is mostly
sandy clay: the line I have taken for the boundary is where this
doubtful stuff ends and the purer sand begins. It must be remem-
bered that it is within quite narrow limits that its right position is
doubtful. Beyond Three Bridges Station the change from clay to
sand becomes more marked again, and keeps so till near Horsham,
where there is some difficulty in pointing out the exact boundary.
It is clear, though, that the sand does not extend more than a mile
beyond that town, but, dipping gently westward, disappears beneath
the Weald Clay, the boundary-line changing its direction and trend-
ing to the south-east.

2. Tunbridge Wells Sand, Upper and Lower, with the intermediate
Grinstead Clay.—Of the Tunbridge Wells Sand, we will first speak
of the upper half. The bed of rock-sand at the top of it continues
for some miles; it forms a fine line of rocks at Redleaf, Penshurst,

1861. ] DREW—HASTINGS SAND. 281
and is again exposed in Chiddingstone Park. West of this, for a few
miles, the outcrop of this part of the series is interrupted by some
faults. At Stamford End, Edenbridge, rock-sand is again seen at
the horizon that I am speaking of: but this is about its last point ;
for further west the top of the Wells Sand is thin-bedded sandstone,
with some loam interstratified; and of this same description is all
the upper half of this division. Taking the Tunbridge Wells Sand
as a whole, near the place it is named from, I find, on tracing it west,
that a bed of good stiff clay appears in it, and gets thicker and thicker
the further one goes in that direction. This clay, which I call
« Grinstead Clay,” is first seen distinctly in Penshurst Park and in
the road-cutting that runs along the west side of it. Here I mea-
sured a thickness of 17 feet of clay, and I saw below it a bed of white
rock-sand; while the Wadhurst Clay is not far beneath. Near
Tunbridge Wells itself there is here and there some red, rather loamy
clay, with thick-bedded sandstone beneath it; and this I take to be
the same Grinstead Clay thinning out and occurring only in patches,
while I refer the lower bed of rock-sand that I, some way back,
said there was in the lower part of these sands, to the horizon of that
which underlies the “Grinstead Clay” at Penshurst. It will be.
remembered too that I mentioned a thin varying bed of clay, some of
it red, resting on a bed of rock-sand or thick sandstone, as occur-
ring about Cranbrook; this is probably the equivalent of it too.
Following the same bed westward for some miles, I see little of it
on the north, on account of the faults; but more to the south a suc-
cession of outliers enables us to get a good idea of it. North of
Hartfield it may be 20 ft. thick; at the most easterly of some out-
liers that occur north of Forest Row it is 30ft.; at the next some-
what more than that is seen, though the top has been denuded ;
while at East Grinstead the thickness is probably 40 ft.; and here
it is worth while to look more closely into its character. At the
very top of it there is red clay, which is a very useful mark by which
to recognize this stratum; lower down it is brown clay, or brown
shale, or blue shale; it everywhere makes very stiff ground, and it
ends sharply against the sand that is below. This sand, as at Red-
leaf, is either rock-sand or thick-bedded sandstone, in a mass of 30
feet or so thick. Sections of it may be seen in most of the lanes about
East Grinstead; but it is also shown in natural sections at Ashurst
Wood Common, where it forms lines of rocks. In other places, too,
it juts out from the side of the hill, and a few miles to the south, at
a place near West Hoathly that bears the name of “The Rocks,” it
makes two long lines of them—the edges of a projecting angle of ©
ground between two deep valleys, that rival in beauty those of Tun-
bridge Wells; and indeed there is such a resemblance between this
and the groups at the last place, that almost every one would at first
say that they belonged to the same stratum—an error that would
probably be confirmed on the finding of a capping of clay to each set.
I have, however, no hesitation in saying that the two beds or their
equivalents are separated by a thickness of strata of more than 100

282 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

feet. This is the conclusion to which I have come after a very
detailed mapping of the ground between the two localities ; and
the Geological Survey Map, which will before long be published,
will show that the course of the beds, though much interrupted by
faults, is consistent only with this theory,—the mass of the Wadhurst
Clay being not far below the rock-bed, and a great thickness of sand
above the clay that rests upon it. There is about 30 feet of sand
that is not rocky, and making only a gentle slope, below the harder
bed ; and then comes the Wadhurst Clay. These changes of the strata
can be best understood by a glance at the vertical section, fig. 1,
p- 276, in which each of the rock-beds is represented by broken lines :
their appearance and dying out, and the relationship of the clays
above them, will be at once comprehended.

About the lower beds in this part I have not much to say; they
have changed so little from what they are at Tunbridge Wells. The
Wadhurst Clay is just the same mass of clay and shale with clay-
ironstone in it (which stone has been dug a good deal near East
Grinstead), and with a little calcareous grit and shelly limestone,—
the whole being from 100 to 130 feet thick. The Ashdown Sand
does not come much west of Ashdown Forest, where I have before
described it: the top of it around some inliers there are on the
north-east of Grinstead is not rocky, but of the ordinary thin-bedded
stone or else of looser sand ; there is, however, a rock-bed lower in the
sands, as well as a subordinate bed of clay; in general character it is
just as before.

There is a gradual dip of the beds from Ashdown Forest both to
the north and to the west, so that the lower beds disappear as we go
in either direction ; the Wadhurst Clay skirts round the forest and dips
down at about West Hoathly ; while the course of the Grinstead Clay
is three miles or so to the west. This bed, however, is again reached
by a deep valley, along which the Brighton Railway has been made,
exposing the best section of it I have seen. At the cuttings at each
end of Baleombe Tunnel the Upper Tunbridge Wells Sand is seen
underlain by purple clay which passes downwards into blue shale.
More than 40 ft. of this Grinstead Clay can be measured on the north
side; and there is probably about 50 ft. of it on the whole; for in
this cutting the bottom of it is not reached: in the southern one,
however, the rock is seen coming from underneath.

V. Nomenclature of the Hastings Sand.

1. Dr. Mantell’s Nomenclature—We are now in a position to com-
pare what I have related with the accounts of Dr. Mantell, and to
discuss the question of what names may be proper for these strata.
As I have before said, Dr. Mantell makes out two sands separated
by ‘‘ Tilgate Beds,’’ which he describes as sand, cale-grit, and blue
clay, in this descending order. I was at first puzzled to know
whether the strata he met with hereabouts were the Tunbridge Wells
Sand with the Grinstead Clay in it, or the two thick sands with the

1861.] DREW—HASTINGS SAND. 283

Wadhurst Clay between them. Tilgate Forest, which he speaks of as
the great locality for the fossiliferous gritstone of his “ Tilgate Beds,”
is upon the uppermost sand of all, even if we take the name to mean,
as indeed it does, a greater space than is so marked on the Ordnance
map; and the neighbouring forest, St. Leonards, is on the same
strata, except that some of the valleys may just reach down to the
Grinstead Clay. I am told that most of the fossils he collected came
from near Cuckfield; and Mr. Hay of the Geological Survey, who has
been engaged upon that part of the country, informs me that they
were got from two distinct beds—one of them the Grinstead Clay,
the other much higher up in the series.

The sands which he named from the village of Worth, near here,
and placed next below the “ Tilgate Beds,”’ belong to what I have
called “ Lower Tunbridge Wells Sand;” while the beds about
Hastings, which were called “ Tilgate” and ‘‘ Worth” by Dr. Man-
tell, are much lower down, and do not come to the surface within
some miles of these places. This misconception (which could hardly
have been avoided without mapping the country step by step between
the two parts, on account of there being no important break in the
series, and almost no lithological difference between the several sands
and clays) renders it, I think, necessary to disuse the names of “ Til-
gate” and “Worth” Beds; and with them must go that of “ Horsted,”
taken from quite another part, and perhaps accurate in itself; since
these, even if they were applicable to this particular neighbourhood,
could not be used for the beds further east without leading to great
mistakes. I will now shortly say why I adopted the names that
T have been using.

2. Reasons for using the Names now proposed.—Taking the eastern
part first: about Tunbridge Wells the upper sands occupy a great
space; they form nearly all the hills near; and their top bed makes
those conspicuous rocks that I have spoken of. I think, therefore,
their name is well taken from that place. The clay beneath them
is chiefly found in the valleys about there; but near the large
village of Wadhurst, about seven miles to the south-south-east,
it spreads over some tolerably high ground, which is indented by
a series of valleys that expose a great thickness of it, and at last
reach down to the sands below; and its position with regard to
these can also be well seen in the cuttings at the ends of the Wad-
hurst Tunnel. I have on these accounts thought it well to take the
name of Wadhurst Clay for the second stratum. The lower sands
make very high ground, are spread over a large area, and show
a very great thickness on Ashdown Forest, which is the central
part of all the Hastings Sand country: no name, I think, can
be better for these than Ashdown Sands. The bed of clay that
appears in the Tunbridge Wells Sand, and thickens to 50 ft. to
the westward, may well be called Grinstead Clay, from its oc-
curring on the north side of the town of East Grinstead, and
making as large a spread near there as anywhere else, and from
its relation to the lower beds being well seen in that neighbour-

Mt

284 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

hood. This clay of course divides the sand into Upper and Lower
Tunbridge Wells Sand.

VI. Weald Clay of the Neighbourhood of Horsham.

I have said that the Hastings Sand occupies the surface hardly
further west than Horsham, dipping beneath the Weald Clay about
a mile beyond that town; in most maps, I believe, it is made to go
some miles further on, and the hills about Horsham are put down
for Hastings Sand. This difference is due to a slight misunder-
standing of the nature of the strata there. The flat on which the
town is built is on the uppermost beds of sandstone, which lie very
flat, but yet dip gently to the north, and west, and south. The hills
around, the most conspicuous of which is that of Den Park, are
chiefly of clay; there is 120 feet in thickness of it; but they are
capped with a hard stratum, which is no doubt the cause of their
standing out as hills. The beds that compose this are not more,
taken together, than 10 feet in thickness. They are clay with two
or three layers of sandstone, which contain large flat masses of cal-
careous grit, just like what occurs in the Wadhurst Clay. Many
quarries are dug in this; and the ripples and other appearances the
hard stone shows, have been described by Mantell, Lyell, and others.
This set of beds oceupies a great space in the form of a table-land
slightly sloping from the edge of the escarpment above Horsham in
the same direction as the dip, the width being in one place as much
as two miles, and varying from that down to 100 yards. I should have
some hesitation in thinking that all this ground was occupied by a
stratum no thicker than what I have said, but that Mr. Hay (who was
the first to perceive its true position) and myself have traced its
upper and lower boundaries for many miles, and have examined every
section of it without finding any evidence of, or any necessity for
supposing, a greater thickness than I have named. If, therefore, a
division is made into Weald Clay and Hastings Sand, this Horsham
stone must, at least for the north side of the Weald, be included in
the former; for here it is only a 10 ft. bed 120 feet up in the clay,
and further east there is nothing but clay at the same horizon ; for,
as we go away from Horsham in that direction, the feature it makes
becomes less important, and the stone is little worked, and eyvi-
dently thins away: the last signs of it are at Crawley. Behind (on
the north of) the course of this bed from near Horsham to Crawley,
there is another line of hill which might easily be mistaken for the
feature of the Horsham stone ; it is in fact, although of greater alti-
tude than any made by this stratum, entirely of clay, which is yet
higher in the series, the Horsham stone making a step projecting
from beneath it. The thickness of Weald Clay above the level of
the stone-bed is very great indeed; I reckon it to be about 500 feet,
which will give altogether 600 feet or so for the Weald Clay here,
the same as its thickness was found to be in Kent.

1861. | DREW—HASTINGS SAND. 285

VII. Conclusion. Lnthological Characters of the Hastings Sand.

To conclude: I should like to give a short summary of the gene-
ral character of the formation, and to call attention to those points
by a study of which we may get a fuller knowledge than we now
have of the sources of the material of which it is composed, and the
conditions of its deposit.

Plainly divided (as the Wealden formation is, in spite of the ad-
mixture of the two substances to some extent through all its parts)
into clayey beds and sandy beds, we shall find in each of these certain
details that are worthy of notice. The clay is generally shaly,
not hard, but in soft fine lamine; these are sometimes, though not
generally, separated by an accumulation of the cases of Cyprides:
the thinness of the flakes made Prof. EK. Forbes give the substance
the very expressive name of “ paper-shales.” At some parts, how-
ever, there is a mere mass of clay without any stratification seen.
T believe it is always so when the clay is of that crimson-red colour,
ranging from that to purple, which occurs at some definite horizons ; —
the origin of which, whether existing so in the rocks from which the
clay was derived, or acquired more lately, I should much like to hear
accounted for. The clay strata, as before said, are varied with oc-
casional bands of calcareous matter, either pure, as shelly limestone,
or mixed with a large proportion of sand, and making a calcareous
sandstone. Lastly, it contains irony matter, sometimes in the form
of concentrically flaking nodules of brown iron-ore, but more often
as layers of nodules of clay-ironstone.

Of the sandy beds there is more to be said. The sand itself is
nearly always extremely fine, almost an impalpable sand. On this
account it bears itself somewhat in the same way that clay does as
regards the presence of water : instead of absorbing it like an ordinary
sand, it becomes a pasty mass that can be moulded like a very light
clay, and this though it contains no alumina. In appearance, as
well as to the touch, it a good deal resembles the “ Loess” of the
Rhine. The roads that are made with the soft sandstone are in dry
weather thick in dust, but after a good deal of rain in a complete
slush of mud. A small proportion of clay mixed with this, as it is
in many of the loams that are met with in this formation, makes one
think the compound to be much more clayey than it really is.
Sometimes a coarser sand occurs, and this is found more useful for
building-purposes, from its having the quality of sharpness; and less
frequently there are layers of pebbles in the sand, usually about the
size of a pea, but now and then as large as a walnut. I have found
this coarse deposit and the less than usually fine sand generally in
one of the beds of rock-sand. And here I would remark (but I do
not know if the fact is of any import) that these rock-beds in almost
every case of their occurrence underlie one of the beds of clay.
Hydrous peroxide of iron occurs in small quantities in the sand-
stone, generally in thin wavy flakes, sometimes more diffused, so as

286 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6
>)

to make a ferruginous sandstone ; and occasionally clay-ironstone is
seen. Lignite is found in the sandy beds, either in small fragments
scattered through a sandstone or loam, or in a bed, from a fraction
of an inch to a foot or more thick, which does not continue for very
many yards; and, again, there may be carbonaceous matter diffused
through a layer of loam or of clay. Loam occurs in large quantities
_ in the sandy beds; it is in beds some feet thick, interstratified with
the sandstone; the two substances interchange along the same stra-
tum-level, the beds varying very much within short distances. I
think that few continue for long of the same character, so as to be
recognized. Figs. 3 and 4 are two sketches of sections which show
plainly how the changes take place, either by the thinning off of a bed

Fig. 3.—Section in the Tunbridge Wells Sand, near Strawberry Hill,
Tunbridge Wells.

a, a. Sand in lamine. b. White Sandstone, 33 feet. c, c. Sandstone.

Fig. 4.—Section in the Ashdown Sand, at Riverhall, near Frant.

a. Rock-sand. =. Loam in laminz. c. Sandstone. d. Shaly Sandstone.

and the wedging in of a new one, or by the overlying beds lapping
over its edge and occupying what would be its place if it were con-
tinued.

Lastly, the sand often shows oblique lamination in different di-
rections; and it probably was accumulated in that way in other
cases where there are no signs of it from the deposit being homo-
geneous. Ripples, too, are frequent, often well-marked, and Striking
in various ways.

But notwithstanding these changes, it holds good that the beds
which, on the whole, are sandy, and the beds that are chiefly of clay,
lie in the order which 1 have described, as represented in the section,

fig. 1, p. 276.

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 287

2. On the Puritan Rocks of Sourn Yorxsurre; and on their
PaLmontoLoetcaL Retations. By James W. Kirxsy, Hsq.
(Communicated by Thomas Davidson, Esq., F.R.S., F.G.S.)
[Puare VII.]

ConrTeEnrTs.

§ I. Introduction.

§ IL. Permian District in South Yorkshire.
Sections near Doncaster.

1. Bunter Schiefer. 3. Small-grained Dolomite.
2. Upper Limestone or Bro- 4. Lower Limestone.
therton Beds and Lower 5. Rothliegendes or Lower Red Sand-
Red Marl. stone.
§ III. Comparison of the Permian Strata of South Yorkshire with those of
' Durham.
§ IV. Remarks on the Permian Fossils of Yorkshire.
1. Cephalopoda. 5. Polyzoa.
2. Gasteropoda. 6. Entomostraca.
3. Conchifera. 7. Foraminifera.
4. Brachiopoda. 8. Alge.

§ V. Distribution of the Fossils.
A. Fossils of the Lower Limestone.
1, Fossils at Moorhouse. 3. Fossils near Broadsworth.
2. Fossils at Hampole. 4, Fossils near Pickburn.
B. Fossils of the Brotherton Beds.

§ VI. Permian Fossils of South Yorkshire compared with those of Durham.

§ VII. Permian Fossils of South Yorkshire compared with those of Lancashire.
§ VIII. Permian Fossils of Ireland.
§ IX. The Zechstein.

§ X. Distribution of the Permian Fauna in Time.

§ L. Introduction.—In the present communication I propose to
speak of the geology and paleontology of the Permian strata that lie
between the towns of Pontefract and Knottingley, on the one hand,
and Tickhill and the village of Maltby, on the other. In doing so
my chief objects are, first, to endeavour to determine the equivalency
of the subdivisional groups of these strata with those of the adjoin-
ing county of Durham; and second, to throw some additional light,
if possible, upon the distribution of Permian species south of the
Durham area. Towards the accomplishment of these objects I have
made two visits to the district in question—one in 1854, and the other
during the summer of 1859.

Prof. Sedgwick has already described the geology of this region in
his admirable memoir ‘‘On the Geological Relations and Internal
Structure of the Magnesian Limestone*.” Prof. Phillips has also
noticed some of its features in a short paper “On the Geology of
Ferry Bridge and its Vicinity,’”’ published about the same period as
the preceding. And since the publication of these papers, Mr. H.
Clifton Sorby and Mr. Edward W. Binney appear to have pursued
investigations in the same district, though the results have not been
published¢. Sir Roderick Murchison has also alluded to certain points
of its geology in the last edition of < Siluria§.’

« Trans. Geol. Soc., 2nd ser. vol. iii. pp. 87-124.

i Philosophical Magazine, vol. iv. 1828.

¢ See Prof. King’s remarks on Mytilus squamosus, Bakevellia antiqua, and
Dentalium Sorby, Mon. Perm. Foss. pp. 160, 170, 218.

§ Siluria (1859), pp. 348, 349.

VOL, XVII.—PART I. x

288 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

The continued researches that have been pursued of late years in
the Permian strata of Durham have carried our knowledge of their
paleontology and geology much in advance of that of the Permian
formation of Britain generally ; and nowhere is the contrast greater
than with the Yorkshire portion of that formation, more particularly
in regard to its paleontology: and it is with a desire to add
something to what we already know of the Permian strata of the
district specified that I make the following observations. The ex-
haustive investigations of Prof. Sedgwick, however, have left little to
add to the full account of the lithology of this district given in his
memoir ; so that I am obliged to confine my attention chiefly to its
palzeontology. It is a delicate, and certainly a difficult, matter to
notice its geology at all after Prof. Sedgwick ; and I only do so some-
what briefly in order to show how it would seem best to co-ordinate
the subdivisions of strata with those of the Durham series, and for
the sake of more fully explaining some of the facts relating to the
fossils.

$ IL. Permian District in South Yorkshire-—Before proceeding
further, it may be remarked that, in examining a geological map, the
Permian strata of Yorkshire are seen to traverse the centre of the
county in a long narrow stripe, running about N.N.W. and 8.8.E.,
apparently almost wearing out in the former direction, and gradually
increasing in width towards the south until a maximum of about five
miles is attained, at which width they continue into Nottinghamshire.
Their western boundary—most ably described by Sedgwick—ausually
forms a well-marked escarpment, often of comparatively great eleva-
tion above the low-lying plain of the coal-measures to the west*.
Their eastern boundary, where they dip beneath the Triassic strata,
is more difficult of determination, being often masked by alluvium or
marsh-land. As the general dip of the strata is easterly, their order
of succession can easily be examined by passing transversely across
their outcrop. This I did repeatedly during my peregrinations in
this region, and always found the same sequence of beds.

Sections near Doncaster.—In going west from the town of Don-
easter, which stands on the alluvium-covered western edge of the
New Red Sandstone, the first rocks we meet with are some thin flagey
beds of limestone, with occasional bands of red and green marls,
which, as a group, we readily recognize as the “ Brotherton Beds”
of early geologists. After passing extensive quarries of this lime-
stone (which, by the sinking of wells and other artificial excavations,
is known to have a deposit of marl and gypsum at its base) we come
to an extensive series of thick and irregular beds of limestone of a
whitish or yellowish colour and a subcrystalline texture. These beds
form a group of much greater thickness than the preceding member,
and are described by Prof. Sedgwick under the name of the ‘‘ Small-
grained Dolomite.” Still further west we meet with a series of piso-
litic, cellular, arenaceous, and compact limestones, some of which are
fossiliferous. The lower beds of this latter group rest immediately

* As at Barnborough Cliff, Hooten Pagnell, and several other places, where
the prospect westward is most magnificent.

1861. ] KIRKBY—PERMIAN, SOUTIL YORKSHIRE. 289

upon a deposit of false-bedded, incoherent sandstone, which it is not
difficult to identify as the Lower Red Sandstone or Rothliegendes.
Beyond this are the Coul-measures.

There are several routes.across the outcrop of the beds, with Don-
caster for the starting-point, that show this succession of strata. It
is well shown on the south side of the Don on the road leading by
Hexthorpe, Warmsworth, and Conisborough to Hooten Roberts, and
on the north bank of the same river along the road by Newton
and Sprotborough to Cadeby,—the numerous quarries on each route
aftording a good general section. A magnificent section is to be ob-
tained by traversing the valley of the Don from Doncaster to a little
beyond Conisborough; and yet another, and one of the best, which
Sir Roderick Murchison has already noticed*, on the South Yorkshire
Railway between the points last-named. In all these lines of section
the same superposition occurs,—and not only here in the valley and
on the banks of the Don, but north as far as Pontefract, and south
to Roche Abbey, which are the limits of the district I have examined.
North of the Don an excellent section is to be obtained in the Vale
of Went, from east of Little Smeaton to Wentbridge; and to the
south there is one almost equally instructive from Tickhill to Maltby.

From the investigations of Sir Roderick Murchison and the officers
of the Geological Survey, it would appear that there are some beds of
red sandstone and marl overlying the Brotherton Limestone of this
district, which also belong to the Permian formationy. And, though I
have not been able to identify these beds myself, I include them in the
following list of subdivisions as the uppermost member of the Permian
series of South Yorkshire on the authority of these observers.

To recapitulate, then, the Permian series of South;Yorkshire seems
capable of being naturally divided, in the descending order, as fol-
lows (see fig. 1) :—

1. Bunter Schiefer.

2. Upper Limestone—ineluding the Brotherton Beds
and Lower Red Marl and Gypsum.

3. Small-grained Dolomite.

4. Lower Limestone.

5. Lower Red Sandstone.

As Prof. Sedgwick has already described the physical geology of
these subdivisions, it will scarcely be required of me to notice them
at any great length. It is requisite, however, that I should give a
description of these strata as far as necessary for their features to be
understood, and for the proper appreciation of their relations to each
other and to the subdivisions of the Permian group of Durham. For
fuller descriptions I refer the reader to the memoir of Prof. Sedgwick
in the ‘ Transactions’ of this Society for 1835.

1. Bunter Schiefer.—Soft red sandstone and marl (Murchison and
Geol. Surveyors).

2. Upper Limestone or Brotherton Beds, and Lower Red Marl.—
The Brotherton Beds are a series of thin, flaggy limestones, usually
hard and compact, and of a yellow or grey colour. The surface-

* Siluria, p. 348. + Siluria, p. 526, and Table of Strata, p. 432.

290 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

planes are generally a little apart, and often coated with red, green,
or purple clays or marls ; bands of marls similarly coloured are occa-
sionally met with among the limestones (Hexthorpe).

Fig. 1.—Sketch-section of the Succession of the Permian Strata in
South Yorkshire.

Coal- New Red
measures. Sandstone.

c d e€

ED
f. Bunter Schiefer. _ ¢. Brotherton Beds. d. Lower Red Marl and Gypsum.
e. Small-grained Dolomite. b. Lower Limestone.

a. Rothliegendes or Lower Red Sandstone.

In certain localities some of the beds contain casts of Awinus
dubius and Myalina Hausmann, together with some obscure remains
that seem referable to Alga.

The Lower Red Marl and Gypsum immediately underlie the pre-
ceding beds. They consist of beds of red and variously coloured
marls with bands of gypsum, are apparently unfossiliferous, and
are rarely seen in section.

‘The slight importance which the Lower Red Marl seems to hold
in the physical geology of this district, the absence of any paleon-
tological feature belonging to it, and the occasional presence of red
and other coloured marls in the Brotherton Beds have induced me to
describe it along with the last-named deposit, and to suggest the
propriety of considering it as part of the same subdivision. I do
this with much diffidence and some doubt, being aware that such a
view is opposed to the opinions of Prof. Sedgwick and the officers of
the Geological Survey.

The Brotherton Beds are well exposed at Knottingley, Womersley,
Hexthorpe, Wadworth, and many other localities, bemg much worked
for hme-burning and road-repairs.

3. Small-grained Dolomite.—A crystalline, subcrystalline, or
compact limestone of a slightly yellow, cream-coloured, whitish or
lustrous grey tint. Thickness of beds ranging from 3 feet to
1 foot and under. Stratification very irregular, beds thickening to
maximum, and thinning out suddenly; it being almost the excep-
tion for one stratum to appear in section for a moderate distance:
planes of stratification curiously pitted. Among the uppermost beds
occur intercalations of greenish clay or marl a few inches thick (Chiff
Quarry, Brodsworth).

This limestone seems to be entirely void of fossils, except inferiorly
towards its junction with the Lower Limestone, where faint traces of
them occur (Town Quarry, Conisborough); and in these lowest beds
there is also a tendency towards an oolitic character, that is never
to be observed in the middle and upper parts, though much less
evident than in some of the beds of the Lower Limestone.

The very peculiar stratification of the Small-grained Dolomite is

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 291

mentioned by Prof. Sedgwick as having been noticed by him at
Steetly, near Mansfield, and other places*. It is a common charac-
teristic of it generally. In the old quarries at Warmsworth sections
most illustrative of this character are to be seen, one of which is
represented in the accompanying woodcut.

Fig. 2.—Sketch of the False-bedding in the Small-grained Dolomite
at Warmsworth Quarry, near Doncaster.

The different beds are interwoven as it were, and form about as
curious a piece of undisturbed stratification as it is possible to con-
ceive. Beds which have a maximum thickness of 2 feet actually thin
out in each direction within a space of 20 feet, their places in the
section being taken by others almost equally brief in continuance.
It is thus difficult to trace a line of bedding for any great extent ; and
within the traceable extent even of the most continuous beds the
line is often a curved one of great irregularity. Indeed some of the
sections in the Warmsworth Quarry‘, as well as in others, are neither
more nor less than highly illustrative instances of false-bedding—a
character common enough in arenaceous deposits, but very unusual
in limestones. .

Another peculiar feature of this limestone is the manner in which
its planes of stratification are pitted—almost as though worked by an
artist, Prof. Sedgwick likening it to “ artificial rustic workt.” These
surfaces are covered as thickly as possible with little pits or hollows,
that extend for Ith or 1th of an inch into the limestone, with dia-
meters of about the same measurements (that is, when largest), their
depth and width often being much less. I have little doubt myself
of this feature being due to some peculiar concretionary action, ana-
logous to that which gave the Upper Limestone of Durham its
remarkable structures.

For architectural purposes the limestone of this member is perhaps
unequalled in England. It can be obtained in blocks of any moderate
size, has a texture and hardness highly suitable for delicate mason-
work, is of a beautiful tint, and will withstand almost any amount of
weathering. It is therefore scarcely to be wondered at, that many of
the finest edifices in England are constructed of it. Its quarries

* Trans. Geol. Soc., 2nd ser. vol. iii. p. 84.

t The quarry here referred to lies at the west end of the village, and just to the
south of the main road leading to Conisborough.

{ Trans. Geol. Soc., 2nd. ser. vol. iii. p. 84.

292 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

of Huddlestone, Bolsover, Steetly, and Roche Abbey are amongst the
most famous in the country*.

Its maximum thickness must be about 200 feet or more. This
thickness it would appear to attain on the right bank of the Don, a
little to the south of the river. In other places it cannot be near so
thick, as between Hampole and the Great North Road; indeed, the
variability in the amount of space between the outcrops of the Bro-
therton Beds and the Lower Limestone, allowing for difference of
position in surface, indicates a great variability in its thickness in
its north and south range. For this reason, and on account of its
irregularity of bedding, I am disposed to look upon it as having ori-
ginated in a comparatively shallow sea. Its general structure im-
plies the influence of currents of great inconstancy, and altogether
reminds us of that which may be supposed to characterize those sub-
marine banks, such as the “ Dogger Bank” of the German Ocean,
that accumulate in water of no great depth, under the influence of
variable currents, at some distance from land.

The Small-grained Dolomite can be easily examined in numerous
localties west of Doncaster, where it is well exposed in the pictu-
resque crags of the Don, and in the quarries that have been opened on
the banks of that river. Amongst other localities may be named the
quarries at Warmsworth, Levit Hage, Cusworth, Outmoor, Cockhill,
Sprotborough, Roche Abbey, and Brodsworth ; the cliffs in the Vale
of the Went, and on the banks of the Don east of Conisborough.

Professor Sedgwick notices it as occurring also at Mansfield, Bol-
sover, and Steetly further south, and at Huddlestone, to the north of
these localities.

4. Lower Limestone.—Between the beds just described and the

* Tt should be remembered, however, that even this limestone, like all other
rocks of sedimentary formation, requires selection; for intercalated among the
beds of good stone are others which do not possess the most important property
of capability to withstand atmospheric action. And not only so, but it is exceed-
ingly difficult to distinguish such beds from the best. It thus happens that a
certain percentage of stone of an inferior quality is often supplied to the builder
along with a large quantity of good, and is used by him without suspicion of
the evil. I saw an illustration of this in the new church of St. George at Don-
caster, which is chiefly built of this limestone, where the surface of stray blocks
in the exterior was already in a state of decay when I visited it only one year
after it had been opened. Much of the stone used in the erection of the New
Houses of Parliament is from quarries (Huddlestone and Bolsover) of the Small-
grained Dolomite; and it would seem as if stones from its worst beds had been
supplied rather extensively. For I cannot think that stone from its best beds
would ever have shown such signs of decay as it is asserted the stone of the river-
front of the palace already shows, even if we allow the atmosphere of the me-
tropolis to be very deleterious indeed. And, notwithstanding all the obloquy that
has been thrown upon the parliamentary commission appointed to select the
building-stone for fixing upon a magnesian limestone, and this in particular, there
can be no doubt they were right in their choice—the fault not being in the stone
chosen, but apparently in the neglect of the architect in not seeing that it was
taken from the right beds. To obtain a good supply of stone of uniform good
quality, it is necessary to appoint some one at the quarry to select the beds to be
worked, and to see to the honesty of the contractor or quarryman in working only
those selected,—the only difficulty being the requisite knowledge to deternfine
which are the superior ; and this, I conceive, is rather to be attained by long prac-
tical experience than from experiments in the laboratory.

1861. ] KIRKBY—-PERMIAN, SOUTH YORKSHIRE. 293

Rothliegendes is a series of limestones of various characters whick
may be conveniently grouped us the Lower Limestone. Some of these
are oolitic, pisolitic, and nodulous (Brodsworth, Moorhouse, &c.) ;
other beds may be termed polyzoan, being almost solely composed of
fragments of Polyzoa (Brodsworth, Cadeby, &c.); others are cellular
and unstratified (Pontefract); and others, again, are compact (Hickle-
ton, Conisborough, &e.), or arenaceous (Bag Hill, Pontefract, Barn-
borough Cliff). Perhaps there is no single section of the Lower Lime-
stone that shows the whole of these beds, though by examining a
mile or two of the escarpment, or a few transverse sections of the
limestone west of the Small-grained Dolomite, limestones of all the
characters mentioned may be met with, besides others that are more
or less modifications of these. In the vicinity of the Don the upper
portion of this subdivision is a soft, thick-bedded, yellowish, oolitic
dimestone,—the roe-like grains being in some beds intermixed with
irregularly rounded concretions as large as peas, and in others with
concretionary nodules an inch or more in length, it being not un-
common to find the same stratum oolitic, pisolitic, and nodulous.
Several species of fossils occur in these beds, generally as casts. A
little lower down are some thick beds equally as soft as the former,
which are chiefly composed of comminuted Polyzoa, principally of
the species Acanthocladia anceps. Beneath these and immediately
above the sandstone are other beds, which are thinner, darker-
coloured, and more compact, or rarely earthy. Numerous remains
of a few species of fossils occur in these beds, but often most imper-
fectly preserved *.

In other places more to the north, especially about Pontefract and
at Wentbridge, the upper part of this subdivision is soft, yellowish,
amorphous, and full of irregularly shaped sparry cavities. Under it
are some thick beds of a harder limestone in which are immense
quantities of Gervilliw (casts). Below these are some thin strata of
hard, compact, pisolitic, and arenaceous limestones, charged with
the remains of Avinus dubius and Gerviilia antiqua. These latter
beds are seen to rest upon the Rothliegendes at Bag Hill, opposite to
Pomfret Castle, where they become arenaceous and almost graduate
into sandstone.

The junction of the lower beds of imestone with the Rothliegendes
can be seen to great advantage in several sections in and about Pon-
tefract, as Prof. Sedgwick has pointed out. It can be well studied
in section to the south-west of the town in some road-cuttings and
quarries, particularly in one on the Carlton and Ackworth road.
Another interesting section is to be seen in an obscure old quarry on
the escarpment, just above the pretty little hamlet of Carlton, where
the lowest limestone, which is cellular, void of stratification, and
charged with a few badly preserved fossils, rests upon an irregular
surface of the sandstone, the latter being yellowish, moderately hard,
and false-bedded. The lowest limestone in this instance appears to

* Prof. Sedgwick describes the most characteristic of these beds in section ix.

of his “Great Middle Deposit of Yellow Magnesian Limestone.” Trans. Geol.
Soe., 2nd ser. vol. 11. p. 93.

204 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

be the equivalent of the amorphous limestone previously mentioned ;
and from this we infer that the beds found beneath that deposit in
some of the sections about Pontefract are here wanting.

One of the most interesting sections illustrative of the junction of
the lower limestone with the Rothliegendes is at Wentbridge, in
the cutting on the Great North Road. The latter deposit is here —
seen towards the south end of the cutting, forming a large portion of
the cliff on each side of the highway, and capped by a few feet of
limestone, which, by the ascent of the road and the dip of the beds,
gradually increases in quantity to the north-east—the sandstone
disappearing, and fresh beds of limestone coming in that direction.
The beds of limestone immediately above the sandstone are thinnish,
of a brown colour, compact in texture, and contain the remains of
Aginus dubius and Gervilla antiqua. These strata occupy a few
feet of the section and are superimposed by a stratum of hard lime-
stone about 6 feet thick, full of the casts of G. antiqua. Other
massive beds follow, some of which are fossiliferous; and above them
are some thinner beds of soft and friable limestone, also with casts
of Gervillia.

On other parts of the escarpment, as at Hampole Stubbs*, the
Rothliegendes is covered by some thick beds of reddish limestone of
a compact, subcrystalline, or oolitie character, and which contain
several species of fossils, among others Aaimus dubius very large.
But in this section the oolitic beds of the member occur much nearer
the sandstone than in other places to the north and south.

Another section showing the two deposits in juxtaposition is found
on the escarpment between Hooten Pagnell and Hickleton, where a
series of thin-bedded, hard, crystalline, unfossiliferous hmestones of
a brown colour are seen to rest immediately upon the Rothhegendes,
which is here soft and very incoherent. The structure of these lime-
stones rather resembles that of the Brotherton beds, the strata being
of similar thickness and hardness as those of that member. Asa
section of the Lower Limestone it certainly differs most widely from
any other that I met with on the escarpment or elsewhere in South
Yorkshire +.

Viewing the Lower Limestone as a whole, we perceive it to be
more inconstant in structure, composition, and general character,
than any of the other subdivisions of the series. The sections just
noticed suffice to prove its mutability; and more comprehensive
details would only tend to make the fact more evident. Neverthe-
less, though the most variable member of the Permian formation in
South Yorkshire, it can always be easily distinguished from either of
the limestone members that overlie it, its features being peculiar and
well marked.

Most of the limestones of this group are included along with the

* The locality of Hampole Stubbs, which is on the road leading from Don-
caster to Wakefield, and just beyond Little John’s Well, would seem to be
identical with the ‘ Stubbs Hill” of Sedgwick.

+ This section occurs in a plantation scarcely a mile south of Hooten Pagnell,
and near to a footpath that winds along the escarpment from that village to
Hickleton.

1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 295

Small-grained Dolomite in the third subdivision or “ Great middle
deposit of Yellow Magnesian Limestone *” of Prof. Sedgwick. Some
of the most inferior appear to be placed in his second subdivision,
the “‘ Marl-slate and thin-bedded and nearly compact limestone f”’.

The organic remains of this subdivision possess considerable inter-
est, as our knowledge of the distribution of the Permian fauna in this
area is almost solely based upon them, there being but three species
of the Yorkshire list that range beyond its limits. The state of
preservation of the fossils is generally as casts, it being exceedingly
rare to meet with examples in a more perfect condition. Their
extreme abundance—at least of certain species—on some horizons has
been alluded to in the cases of Wentbridge and Brodsworth. And
so far as we may judge, this abundance extends over comparatively
wide regions; for in the case of the Gervillia-bed, which occurs so
thick at Wentbridge, I have traced it over a distance of twelve miles,
having seen it also at Pontefract (Bullhill Quarry), Emsall, Hooten
Pagnell, Brodsworth, Hickleton, and Barnborough Cliff. The polyzoan
beds I have not traced so far; but they are to be found at Brodsworth
(Freestone Quarry), Hampole, and Cadeby. Further particulars of
the fossils of this member will be given in another part of the paper.

As an approximation, 120 feet may be given as the probable thick-
ness of the Lower Limestone ; it being questionable whether it ever
exceeds that estimate, though scarcely so as to whether it sometimes
reaches it.

Amongst other localities affording good opportunities for studying
its various beds, may be mentioned the numerous sections alluded to
in the neighbourhood of Pontefract, which illustrate the cellular and
arenaceous forms of it; and the quarries at or near Brodsworth,
Hampole, Hampole Stubbs, Emsall, Conisborough, Cadeby, Moor-
house, Hooten Pagnell, and Hickleton the oolitic, polyzoan, and
compact beds.

5. Rothliegendes or Lower Red Sandstone.—A deposit of yellow,
red, grey, or variegated sandstone; fine-grained, or rather coarse in
texture; of irregular structure, false-bedding bemg common; and
though sufficiently firm to form a soft building-stone in some locali-
ties (Pontefract, Barnborough Cliff, and Wentbridge), yet often very
soft and incoherent (Wentbridge, Moorhouse, and Hickleton).

The Lower Red Sandstone of South Yorkshire differs little from
that of Durham, except, perhaps, in being a little more coherent and
finer-grained. And in no case have I observed any decided instance
of its unconformability to the overlying limestone, though it is not
always easy to say whether it is conformable or not, its stratification
being subject to such irregularities. There is no section on that
portion of the escarpment I examined that affords much support to
the opinion of those who would separate it from the Permian strata
on account of its unconformability to them—rather to the contrary.

This deposit is so well described by Prof. Sedgwick that I would
rather direct attention to his remarks on it than attempt further
description. It is easy of examination along the escarpment in

* Trans. Geol. Soc., 2nd ser. vol. ili. p. 81. + Loe. cit. p. 79.

296: PROCEEDINGS OF THE GEOLOGICAL SOCIDTY. [ Mar. 6,

South Yorkshire ; and it is nowhere better exposed, nor more charac- .
teristically developed than about Pontefract *. In quarries on the
north and west of that town it is worked as a building-stone, being
of about similar coherency as the equivalent beds in the vicinity of
South Shields, which are likewise used by the builder. Among
other localities on the escarpment south of Pontefract, may be named
those at Carlton, Wentbridge, Hampole Stubbs, Moorhouse, Hickle-
ton, Barnborough Cliff, Cadeby, &c.

§ III. Comparison of the Permian Strata of South Yorkshire with
those of Durham.—Having now given some details illustrative of the
characters of the subdivisions of the Permian series of South York-
shire, it will be of interest to attempt their co-ordination with the
subdivisions of the equivalent series of Durham.

Commencing at the base, we have the lower red sandstone, the
equivalency of which with the lower red sandstone of Durham, as
well as with the typical Rothlegendes of Germany, has been so long
known to geologists as not to require special pointing out. Indeed the
researches of Prof. Sedgwick clearly show the Yorkshire and Durham
beds to be portions of one deposit, in all probability yet eontinuous.
We have thus contemporaneous subdivisions at the base of each
series. If we pass on to the Brotherton beds, the highest calcareous
member, we find that it agrees in position with the upper limestone
of Durham, and, besides, that it is characterized by the same fossils,
and by a similar paucity of them. For these reasons I look upon
the Brotherton beds as the equivalent of the upper limestone, being
fully persuaded that such agreements could not have occurred in
deposits of different periods. Thus we have the lower limestone and
small-grained dolomite confined between two determined horizons,
with the marl-slate, compact limestone, and shell- and cellular lime-
stone of Durham as equivalents. Of these I look upon the lower
limestone as being parallelized by the marl-slate and compact lime-
stone, and the small-grained dolomite by the shell and cellular
limestone. The marl-slate has no special representative in York-
shire. And, though it is possible that its deposition may have pre-
ceded the commencement of that of the lower limestone, I see
nothing that leads me to suppose that it did. In classing it as the
equivalent in part to that Yorkshire member, I rely upon the fact of
its being the commencement of calcareous beds in the Durham series,
just as the lower limestone is in the series of Yorkshire, and on the
probability of the accumulation of arenaceous sediment having been
consummated and that of calcareous sediment begun about the same
period in both regions. It is the compact limestone, however, that
is to be considered as principally equivalent to the lower limestone.
In regarding the shell- and cellular limestone of Durham as the
equivalent of the small-grained dolomite, it may be objected that
the great difference that exists in their paleontological features is
opposed to such an identification. To this I would reply that the dif-

* The fine deep soil in which the people of Pomfret grow the liquorice-root

to manufacture the “ Pomfret Cakes,” for which, among other things, their town
is so famous, seems to be largely composed of the débris of this member.

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 297

ference is one of distribution, similar to the differences seen in the
distribution of marine life in recent seas—the bottoms of which, we
know, offer many examples of great irregularities in the distribution
of the various forms of life that people them. To conclude, we have
the Bunter Schiefer of Yorkshire apparently parallelized by some
obscure and little-understood beds of red sandstone which occur in
the south-east portion of the county of Durham, superior to the
upper limestone, and which have been classed by Mr. Howse* as
Permian under the name of Lower Bunter.

In arriving at these conclusions I have chiefly been guided by the
relative positions of the subdivisions of each series. Indeed, in this
instance, with such differences in the paleontological and structural
features of the subdivisions, vertical position is almost the only test
that can be used in attempting to parallelize them; and in series of
strata, or rather in portions of the same series so little apart as the
two compared, vertical position would seem to be as good a test as
any that could be used. I would also observe that, in regarding
subdivisions to be equivalents, I also consider them to be of con-
temporaneous deposition. ‘Thus the Brotherton Beds and Upper
Limestone not only represent the last deposition of calcareous sedi-
ment in each area during the Permian era, but are looked upon as
contemporary. It is not, of course, supposed that the accumulation
of each commenced and ceased at exactly the same periods in both
areas, but that the bulk of each subdivision was synchronously
deposited. [See the Tabular View of the Pernuan Strata of Durham
and South Yorkshire, p. 298].

§ V. Remarks on the Fossils ——I now proceed to notice the species
T have met with in this district.

CEPHALOPODA.

1. Navritus Frerestesent, Geinitz, Neues Jahrbuch, p. 637, pl. 11.
fio:
Syns. N. Bowerbankianus, King; and N. Theobaldi, Geinitz.

A cast of a body-chamber of a young individual of this species
occurred at Brodsworth. It is rather less than half-an-inch long, is
a little more compressed medianly than Durham specimens of simi-
lar age, and shows traces of a shallow median sulcation.

This is the only Cephalopod I have met with in Yorkshire; but
Prof. King quotes it from Aldfield, Yorks. (in the cabinet of Prof.
Phillips)r.

GASTEROPODA.
2. Turso neLicrnus, Schlotheim, Petrefactenkunde, p. 161.

Syus. Turbo Mancumensis, T. minutus, and Rissoa obtusa, Brown ;
Tittorina Tunstallensis, Howse; and Turbo Thomsonianus,
King.

Full-grown specimens of this species in Yorkshire have five whorls,

and are about one-sixth or one-fifth of an inch in length. At Ham-

* Ann. and Mag. Nat. Hist., 2nd ser. vol. xix. p. 34.
t Mon. Perm. Foss. of Hngland, p. 220.

PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

298

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1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 299

pole immense quantities of young and probably rather dwarfed spe-
cimens are to be had, some portions of the limestone being literally
full of them; and as all these specimens are testiferous, and many
of them in a perfect condition, they have afforded me a good oppor-
tunity for studying some of the variations of form and character to
which this species is subject. The following remarks are therefore
solely based upon these materials.

The common form is usually as wide as long, with a large body-
whorl, a short, depressed spire (which occupies less than ‘half the
entire length), anda large umbilicus. The whorls are ventricose and
rather flattened behind ; the body-whorl increases rapidly and has
two prominent central ribs, bounded on each side by others of less
strength, which characterize the species; the apex is obtuse; the
aperture orbicular with a slightly reflexed pillar-lip.

Many of the specimens are proportionally longer (the spire being
‘drawn out a little and the body-whorl of less width), and have the
whorls rounder and the spiral ribs of uniform strength.

Another variety is without spiral ribs, or with very faint indica-
tions of them, and has the whorls somewhat shelving behind, most
prominent a little below the median line, and well rounded in front,
with a narrow, flattish region bounding the suture.

There are numerous intermediate forms that are more or less mo-
difications of the three noticed, whose differences they serve to con-
nect by numberless slight gradations. This is strikingly the case
with the differences observed in the strength of the spiral ribs, it
being possible to form series of specimens showing their gradual obli-
teration ; .and so it is with the differences seen in the size of the
spire, and with those of the rotundity of the whorls. Indeed, it is
almost easier to pick out specimens showing some slight differences
than specimens which show none.

The Hampole specimens invariably have a more obtuse apex than
those of Durham, the first and second whorls being flatter compared
with the succeeding ones.

The generic position of this species, like that of several other Per-
mian univalves, is still somewhat uncertain. It has been placed in
Turbo; and its general resemblance to the shells of that genus in-
duces me to allow it to remain there. Its resemblance to Littorina,
to which it has also been referred, is perhaps almost as great. And
it is only right to mention that the operculum of this shell has
never been found, which is better explainable on the supposition of
its being horny, like that of Zittorina, than calcareous like that of
Turbo. There is, however, no instance on record of the operculum
of any of the Permian Gasteropods having occurred in England or
Germany.

Loc. Pontefract, Hampole Stubbs, Moorhouse, Pickburn, Brods-
worth, Conisborough, and Barnborough Cliff. Taken by Prof.
Sedgwick between Marr and Hickleton*; and by Prof. Phillips at
Aldfield ¢.

* Trans. Geol. Soc., 2nd ser. vol. iii. p. 118.
t Mon. Perm. Foss. of England, p. 205.

300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [ Mar. 6,

3. Rrssoa Letent, Brown. Pl. VII. figs. 1-6.
R. Leight, Brown, Trans. Manchest. Geol. Soc., vol. i. p. 64, pl. 6.
figs. 9-11.
Syns. Rissoa Grbsont and R. pusilla, Brown.

Typical specimens of this minute species are ovately conical in ge-
neral form; with four, or rarely five, flatly convex smooth whorls,
that increase quickly in length and width, and which are divided by
a deepish and slightly oblique suture. One half of the length is oc-
cupied by the body-whorl, which has a well-rounded basal slope ;
the spire is conical, with rather a blunt apex. The aperture is
nearly oval and of moderate size, the outer-lip being strongly arcuate,
the pillar-lp somewhat curved, and reflected, with a slight umbilical
chink behind it.

Length + inch; breadth 54.

There are other specimens almost obovate in form, with convex
whorls, more depressed spire and obtuse apex. Others, again, have a
large body-whorl, rounded whorls, and also an obtuse apex.

An examination of a type specimen of Rissoa Gibsoni from the
Lancashire Permian beds (kindly lent me by Mr. Binney) has led me
to place that species along with the one I am noticing, of which it
seems to be but an enlarged form.

The Trochus pusillus, Geinitz, of the Unter Zechstein, is a related
form, but undoubtedly distinct from the present. So it would ap-
pear is the Turbo Permianus, King, of the Shell-limestone of Durham.

Rissoa Leight has only occurred to me at Hampole, where it is not
rare in the beds containing Turbo helicinus. It is found in greater
plenty in the Permian marls and limestones of Colyhurst near Man-
chester*. It has also been met with under its Gibsoni form by Prof.
King, at Tullyconnell*.

4. Turrrretta Atrenpureensis, Geinitz. Pl. VII. figs. 9, 10.

Turbonilla Altenburgensis, Geinitz, Verstein. deut. Zech. p. 7,
tab. ui. figs. 9, 10.

Syns. Loxonema fasciata, King; L. Geimitziana, King; Turritella
Phillipsti, Howse ; T. Tumstallensis, Howse ; and [issoa gracilis,
Schauroth.

Specimens of a minute turreted shell are not rare in the Lower
Limestone at Hampole. Like the individuals of other Gasteropods
from this locality, they are evidently young individuals, and some-
what stunted in growth.

These specimens are minute, turreted, and smooth. They have
only five whorls, rarely six, which increase gradually in length, and
somewhat quickly in breadth. The whorls are ventricose and equally
rounded; the suture is deep, rather wide, and oblique. The body-
whorl is about as long as one-third of the entire length. The aper-
ture, which occupies rather more than one-fourth of the length of
the shell, is obovate, being rounded behind and rather produced in

* Messrs. Binney and Brown in Trans. Manch. Geol. Soc., vol. i. p, 63; and
Prof. King in Mon. Perm. Foss. of England, pp. 205, 206.

+ Journ. Geol. Soe. of Dublin, vol. vii.

1861. | KIRKBY—PERMIAN, SOUTH YORKSHIRE. 301

front; the outer lip is strongly convex; the pillar-lip is slightly
convex, and a little reflected; behind it is a very minute umbilicus
which in some specimens is scarcely observable.

Length ;}, inch; breadth 5), inch.

In the adjoining quarries of Moorhouse and Hampole Stubbs other
specimens of what is evidently the same species occur, twice or
thrice as large as those just described, and with a greater number of
whorls. These specimens are always in an imperfect condition.

These Yorkshire Turritelle agree very well with Geinitz’s figures
and description of Turbonilla Altenburgensis, their general width,
perhaps, being a little less compared with their length. They also
very much resemble the specimens found by Prof. King in the Tully-
connell limestone, and referred by him to this species. There is a
much greater difference, however, between them and the Turritelle
of the Shell-limestone of Durham, as there also is between the latter
and those of Germany. The Durham examples are much more finely
developed, ranging from half-an-inch to an inch in length, and with
from 8 to 12 whorls; their aperture is also different, being more
angulate by the greater straightness of the pillar-lip. Still I think
that the Durham specimens may likewise belong to this species, their
differences being such as we may easily suppose to be due to their
higher state of development. Ido not wish to assert this opinion
with much dogmatism, though it seems the most probable to me:
and I would add that it is in a similar spirit that I class with this
species the various forms indicated by the synonyms at the head of
these remarks. It is my opinion that the whole of them are refer-
able to the present species—it apparently having the right of pri-
ority ; and this is also the opinion of other Permian paleontologists,
whose views are of more worth than my own*. Still it should be
acknowledged that the question is one of some difficulty and not
easy of solution; and that there is, even yet, much to be said in
favour of the specific distinction of some of the forms here included
as synonyms.

5. Cuemnitzt1a Rorsstert, Geinitz, Jahres. Wetter. Gesell. 1850-51.
Syn. Lowonema Swedenborgiana, King, Mon. Perm. Foss. p. 210.

A single impression of a fragment of this species occurred at
Hampole Stubbs. The specimen shows five whorls strongly ribbed
transversely. It is about 1th of an inch in length. The apex is not
shown, neither does the largest whorl of the impression appear to be
that of the body-whorl. Nevertheless the specimen possesses suffi-
cient character to allow the species to be determined,—the form of
the whorls and their transverse ribs being’ unmistakeably those
of C. Roessleri.

This species is found also in the Unter Zechstein and in the Shell-
limestone of Durham.

* See Mr. Howse on 7. Altenbwrgensis in Ann. and Mag. Nat. Hist., 2nd ser.
yol. xix. pp. 446-448; and Baron von Schauroth in Zeitschr. d. deut. Gesell.
1856, pp. 256-244.

302 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

6. SrraParortus Permianvs, King, Mon. Perm. Foss., p. 211, pl. 17.
figs. 10, 11, 12. -

I procured five or six specimens of this species at Hampole. They
are as large as the Durham examples, and have three much com-
pressed and rapidly increasing whorls, a large body-whorl, and a
slightly elevated spire. In the latter respect they differ somewhat
from the majority of the Durham specimens, in which the spire,
though still low, is higher, as it also is in examples from the Unter
Zechstein of Germany. All the specimens are deeply and largely
umbilicated, and have apparently an almost orbieular aperture.

7. Natica mintua? Brown. Pl. VII. figs. 7, 8.
Natica minima, Brown, Trans. Manch. Geol. Soc., vol. i. p. 64,
pl. 6. figs. 22, 23, 24.

Three specimens of a smooth shell with three whorls have oc-
curred to me at Hampole. They most nearly resemble the Natica
minima of Brown. The whorls are ventricose, rather oblique, flat-
tened behind and rounded in front; the body-whorl is very large,
and the spire short; aperture apparently suboval, outer-lip convex,
pillar-lip nearly straight.

The condition of these specimens is not such as will allow me to
speak positively in thus referring them to this species. Nor are the
figures and description given by Capt. Brown such as afford much aid
in their identification. A specimen of the shell, with which I have
been kindly favoured by Mr. Binney, does not look much unlike a
squat form of Turbo helicinus. Nevertheless there is a possibility of
its representing a distinct species; and as there is also a possibility
of these Yorkshire individuals proving to be the same, I refer them
for the present to it—doing so, however, with considerable doubt.

8. Catron Lorrusranvs, King, Mon. Perm. Foss. of England, p. 202,
pl. 16. figs. 9-14.

I have a posterior plate (cast) of a Chiton from Brodsworth, and
an intermediate one (cast) from Moorhouse, which appear to belong
to this species. The former is rather narrow, and has an elevated
and reflexed apex. The latter is obtusely angulated medianly, and
has its posterior and anterior margins almost at right angles to the
dorsal line. The shell of these plates appears to have been somewhat
thick; and the posterior plate, which is the largest, must have be-
longed to an individual about five-eighths of an inch in length.

Two plates of a Chiton are mentioned by Prof. King as haying
occurred in a Permian limestone at Kirkby Woodhouse in Notting-
hamshire*.

9. Denratium Sorsyr, King, Mon. Perm. Foss. of England, 1850,
p- 218. ;
Syn. Dentalium Speyert, Geinitz, Ueber den Zechstein der Wet-
terau, 1852, in the Jahres. der Wetterau. Gesell. for 1850-51.
Not rare in the Lower Limestone at Hampole Stubbs. Specimens
* Mon. Perm. Foss. of England, p. 203.

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 303

are not well preserved, being either casts of the interior, or impres-
sions left in the matrix after the decay of the shell. They are half an
inch or less in length, and are slightly curved, more so posteriorly than
towards the aperture; they taper gradually, and have apparently
been smooth.

Prof. King first described this species from a specimen discovered
by Mr. H. Clifton Sorby at Conisborough.

More than a year ago I found a Dentaliwm in the Shell-limestone
of Durham, which evidently belongs to this species. It is testi-
ferous, of the same length, of similar curvature, and smooth like
the examples just noticed. It perhaps increases a little more rapidly
in width, and is more acuminate posteriorly than they; but these
differences seem of little import.

There does not appear to be much doubt as to this species being
identical with the Dent. Speyert of Geinitz, which occurs in the Unter
Zechstein and Zechstein-Dolomit of Germany. Specimens from these
deposits, sent to me by Baron von Schauroth as those of D. Speyer,
show little variation from English examples. And I have also
compared the latter with drawings of type specimens with which I
have been kindly favoured by Dr. Geinitz, but can detect nothing
that will constitute a specific difference.

Loc. Hampole Stubbs, Conisborough (Sorby).

CoNcCHIFERA.

1. Geryizr1a Antiqua, Minster; Goldfuss, Petrefacten, part 2. p. 126.

Syns. Bakevellia tumida, King; Avicula inflata, A. Binneyi, and

A. discors, Brown.

Two forms of this species occur in Yorkshire. One is longer
than wide, rather inflated, with a shallow curvature in posterior
margin, and a deep byssal sinus. The other is wider than long,
rather flat, and with a byssal sinus not so deep as the first. Neither
is found above half-an-inch wide, generally less. The surface of
both is marked with the regular, finely raised lines of growth so
characteristic of the species in Durham.

The relative thickness of the shell appears to have been greater in
the Yorkshire individuals than in those of Durham. The muscular
impressions and pallial lines are thus often very clearly indicated on
the casts. The hinge-teeth are also very instructively shown in many
specimens.

In one quarry near to Pickburn I obtained specimens of the more
elongate form which assume the character of the Bakevellia tumida
of King,—the valves being very tumid, the hinge-line of great width,
and the shell altogether more irregularly grown than in type speci-
mens of the species.

G. antiqua occurs in immense quantities in the Lower Limestone,
associated with remains of other Gervillie apparently belonging to
the species keratophaga. At Bull Hill Quarry near Pontefract, and
at Wentbridge, their remains almost solely form thick beds of lime-
stone. It is almost invariably in the state of casts, and generally in
detached valves.

VOL. XVIJ.—PART I, Y

304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

It occurs at Bull Hill, Bag Hill, and other localities about Ponte-
fract, at Wentbridge, Hampole Stubbs (Stubbs Hill, Sedgwick),
Hampole, Moorhouse, Pickburn, Brodsworth, Conisborough, Hooton
Pagnell, Emsall, Barnborough Cliff, Cadeby, Braithwell, and near
Micklebring, all localities of the Lower Limestone, and in all of
which it is common.

2. GERVILLIA KERATOPHAGA, Schlotheim, Denksch. Akad. Munch.,
vol. vi. p. 30, pl. 5. fig. 2.
Syn. Bakevellia bicarinata, King.

Specimens of this species occur more rarely than those of the pre-
ceding. They never attain the size of the largest Durham specimens,
though in common with those they possess the same obliquity of
valves, forked posterior margin, and prominent and somewhat distant
lines of growth that characterize the species.

It occurs at Brodsworth, Pickburn, and, I think, in other localities ;
but the preservation of the specimens is such as will not allow me to
speak positively on the matter. Prof. King gives the neighbourhood
of Pontefract as a locality for it.

3. Myatrva Havsmannt, Goldfuss, Petrefacten, part 2, p. 168.

Syns. Mytilus squamosus and M. acwminatus, J. de C. Sowerby ;

and Mytilus septifer, King.

Generally about half-an-inch long, rarely an inch. Not very
common. Occurs both in the Lower Limestone and the Brotherton
Beds, being much dwarfed in the latter.

Loc. Lower Limestone; Bull Hill Quarry near Pontefract, Ham-
pole Stubbs, Barnborough Cliff, near Sprotborough, Conisborough,
Brodsworth, and Moorhouse. Brotherton Beds; Hampole Quarries*,
Knottingley, and Loversall.

4. Myoconcna costata, Brown, Trans. Manch. Geol. Soc., vol. i. p.
32, pl. 6, figs. 34, 35.

Specimens of this species are not rare. They never exceed 2ths of
an inch in length, have generally rather convex valves, slightly curved
dorsal and ventral margins, with well-marked posterior ribs, and the
surface covered with strong lines of growth.

Loc. Brodsworth, Hampole Stubbs, near Barnborough Cliff,
Moorhouse, Hampole, and Bull Hill near Pontefract, all in Lower
Limestone.

5. Carpromorpua Pariast, De Verneuil, Geol. Russ., vol. ii. p. 316.
Syn. C. modioliformis, King.
A single right valve of this species occurred in the Lower Lime-
stone at Brodsworth. It is 2ths of an inch long, is strongly angu-

lated, has its umbone depressed, and appears to have had a very
thin shell.

* “ Hampole Quarries” is the name on the map of the Ordnance Survey for
the quarries on each side of the Great North Road, a little to the north of the
Holmeroyd Bridge and a mile to the east of Hampole village, and rather more
than a mile to the east of the old quarry of Lower Limestone so often mentioned
in this paper as the locality of “ Hampole.”

1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRE, 305

6. Axinus pusius, Schlotheim, Denksch. Akad. Miinch., vol. vi.
p. 31, pl. 6. figs. 4, 5. Pl. VII. figs. 11 and 12.

Syns. Aw. obscurus, Sowerby; Aw. parvus, pusillus, productus,
undatus, elongatus, rotundatus, and Lucina minima, Brown;
Schizodus Schlotheimi, Geinitz; and Sch. truncatus, King.

The most common form of this species in Yorkshire is that which
has been described by Sowerby under the specific name of “‘obscurus.”
Its distinguishing features being already so well known, it will be un-
necessary to notice them in detail. It differs from other varietal
forms of this species in its greater depth anteriorly and in its greater
posterior production, in the convexity of its umbonal region and
larger umbone, in the obliquity of its hinge-line, and (generally)
in the thickness of its shell.

Specimens from some localities—especially those from Moorhouse
—show several deep furrows and ridges in the concavity of the um-
bonal region, running somewhat radiately from the umbone, which
are probably visceral markings. Such examples also generally show
traces of the muscular impressions. These internal markings are,
of course, best seen in specimens with thick shells, and are very
faint or not at all perceptible when the shell has not been of mode-
rate thickness, as at Emsall and Brodsworth. The thickness of the
shell has been quoted as a specific character by those who consider
“obscurus ” a distinct species; but it may be pointed out that, though
the shell of the Yorkshire Aainz is usually much thicker than the
shell of those occurring in Durham, yet its thickness is subject to
variation, just as the size of the shell is variable. Some individuals, and
those not young ones, have the shell little or no thicker than that of
the “ truncatus”’ variety of the Shell-limestone of Durham, whereas
in other cases the shell is fully three times as thick. Thus, instead
of the difference in shell-thickness being of specific value, it would
seem to be merely a difference of individual growth, due probably
to age and locality, which are known to effect analogous results with
the shells of recent Mollusca.

It would appear that Av. dubius attained its maximum develop-
ment in the British area in the sea of the Lower Limestone. It was
there of greater size, more robust, and more prolific than at any
other period of its history. In no other district, and on no other
horizon, in Yorkshire, Durham, or any other part of Britain where
Permian strata occur, does it ever again attain the same size and
abundance. During the same period—while the Compact Limestone
was accumulating—it was a rare species in the Durham area. And
this is a fact worthy of attention: for the two regions are only some
eighty miles distant; yet in one it is the commonest species, and in
the other amongst the rarest.

The Aaini of the Brotherton Beds also belong to the “ obscurus ”
type; but they are there much dwarfed in size, seldom exceeding
half-an-inch in width.

In some localities another variety of this species occurs (figs. 11,
12), which is much smaller than the preceding, its width being only
zyths of an inch. It is almost ovate in marginal ee is regu-

x

306 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

larly rounded anteriorly, and is a little more produced in that direc-
tion than “ obscurus” or any of the other varieties. Its umbone is
comparatively small, and does not extend much above the hinge-
line; the hinge-line slopes gently inwards, and its ventral margin
is regularly rounded and likewise slopes inwards to the posterior ex-
tremity. The valves are regularly convex, and the shell is com-
paratively thin.

This pretty form of Av. dubius is somewhat rare, and has only
eccurred to me in Lower Limestone at Conisborough, Hampole Stubbs,
and Brodsworth.

Loe. In the Lower Limestone at Bull Hill Quarry and other lo-
ealities about Pontefract, at Wentbridge, Hampole, Hampole Stubbs,
Moorhouse, Pickburn, Brodsworth, Conisborough, Hooton Pagnell,
Emsall, and Barnborough Cliff; on Prof. King’s authority it likewise
occurs at Garforth Cliff, Woodhall, and Nosterfield.—In Upper Lime-
stone at Knottingley, Loversall, Wadworth, and south of Robin
Hood’s Well.

7. Macropon srrratus, Schlotheim, Denksch. Akad. Miinch., vol. vi.
p. 31, pl. 6. fig. 3.

Syns. Cucullea suleata, Philips*; Arca tumida, J. Sowerby; A.
antiqua, Minster; A. Loftusiana, Howse; A. Kingiana, De
Verneuil.

Three separate valves of this species have occurred to me in the
Lower Limestone. Their size is very small compared with Durham
examples, being apparently of stunted growth. The largest is half-
an-inch in width.

Loc. Moorhouse, and Holywell Hill (Conisborough).

8. LepA sPpELuNcARIA, Geinitz, Versteinerungen Zech., p. 9, pl. 4.
fig. 6.

Syn. Leda Vinti, King.

I possess two specimens of this interesting species from the Lower
Limestone of Moorhouse. One is a good cast of a right valve with a
portion of the shell adhering to one extremity; the other is a bad
cast of a left valve. The former is about 3ths of an inch in width,
and differs little from Durham specimens, except in being rather
more acuminate posteriorly, and in having the umbonal ridge much
broader and stronger than they.

BRAcHIOPODA.
1. TrrepRatTuLA ELoNGATA, Schlotheim, Denksch. Akad. Miuinch.,
VOL. Vip. 2h Ple (2 He.
Syns. 7. sufflata, complanata, lata, communis, and intermedia,
Schlotheim.

Both the typical form of this species and the variety sufflata occur
in the Lower Limestone, the individuals of both varying in relative
length and width in different localities, but never attaiming so large
a size as in Durham. My largest specimen is half an inch long,

* This is probably the shell noticed by Prof. Phillips, under the name of Cu-
cullea, as occurring in the neighbourhood of Ferry Bridge. See Phil. Mag., new
series, 1828, p. 401.

1861. | KIRKBY—PERMIAN, SOUTH YORKSHIRE.. 307

which is an uncommon length. It is not a rare species at Conis-
borough, where the individuals belong to the typical form; nor at
Hampole, where individuals of both forms occur, though exceedingly
stunted even for Yorkshire.

T. elongata is the only Brachiopod that has been found in the Per-
mian series of South Yorkshire.

Loc. In Lower Limestone at Conisborough, Brodsworth, Hampole,
Hampole Stubbs, and near Wentbridge. It has also been noticed by
Prof. Phillips in the vicinity of Ferry Bridge. .

PoLyzoa.

1. AcantHocrapIA ANcEPS, Schlotheim, Denksch. Akad. Miinch.,
vol. vi. p. 20, pl. 2. fig. 7.

A. anceps is the common Polyzoon of the Permian strata of this
district. It here takes the place—and more than takes it—of the
Fenestella retiformas of the Durham beds. It is usually, however,
much broken up, good characteristic specimens being rare. In only
one quarry (Freestone Quarry) near Brodsworth, have I met with
illustrative examples showing the symmetrical branching of the
stems, and more rarely the celluliferous surface.

Both in the quarry named and in others at Cadeby and Hampole,
the remains of this species form almost the chief bulk of thick beds
of limestone that have long been wrought as a building-stone in the
district a little west of Doncaster. The remains of Acanthocladice
are to be seen studding the surfaces of the weatherworn walls of the
ancient stone buildings of this district. When at Conisborough I
saw it in company with Gervillia antiqua in the stones of the walls
of the castle-keep—probably old acquaintances of Athelstan the
Unready and his compatriots in ‘ Ivanhoe’!

Loc. In Lower Limestone at Brodsworth, Pickburn, Hampole,
Hampole Stubbs, Bull Hill Quarry (Pontefract), and Conisborough.

2. Tuawniscus pustus, Schlotheim, Petrefacten, p. 341.
Syn. Fenestella ramosa, King.

I have taken a specimen of a Polyzoon which very much resembles
this species. It is rather above an inch long, shows the uncelluli-
ferous face, and has a principal stem about 54th of an inch in width,
with many irregular branches almost as wide.

Loc. Freestone Quarry, Brodsworth.

3. Rererora Enrenserel, Geinitz, Grundriss der Versteinerung.,
p- 585, pl. 23. fig. 12.
Syn. &. Lonsdali, Howse; Fenestella Permiana, King.
Interesting fragments of this scarce species occur, along with the
two preceding, in the Freestone Quarry at Brodsworth.

4. Srenopora Macxrotut, Geinitz, Grundriss der Versteinerung.,
p- 582.

Small specimens of simple and branched stems of this species occur
among the débris of <Acanthocladia anceps. In the Brodsworth
Freestone Quarry the examples are always sections, some of which
show the internal arrangement of the cells very clearly, At Hampole

308 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

I have taken it in minute globose and egg-shaped masses, one of
which has a spine-like body for an axis.

Loc. Lower Limestone; Freestone Quarry, Brodsworth, and
Hampole.

ENTOMOSTRACA.
1. CyrHeRE (BarrprA) prepera, Reuss, Jahresbericht der Wetterau.
Gesell. 1854, p. 67.

Syn. C. (Bairdia) curta, Jones (not McCoy).

Several specimens of this species have occurred in the Lower
Limestone at Hampole, and amongst them the varieties elongata,
Neptum, and compressa. Also a single specimen of the variety
ventricosa at the neighbouring locality of Moorhouse.

2. Cyruere (Barrpra) Scuavrorarana, Kirkby, Ann. & Mag. Nat.
Hist., ser. 3. vol. ii. p. 329, pl. 10. f. 14; and Trans. Tynes. Nat.
Field-club, vol. iv. p. 147, pl. 9. f. 14.

A single specimen of this species occurred at Hampole.

3. CyrHErE (Barrpra) ampia, Reuss, Jahresb. Wetter. Ges. 1854,
p> GS, te Ukds dis

A fine example of this species oceurred to me in the Lower Lime-
stone at Hampole, and has been noticed and figured by Mr. Jones
in the Transactions of the Tyneside Naturalists’ Field-elub (vol. iv.
p- 166, pl. 11. figs. 19a, 19 f).

Its only other locality in England is in the Upper Limestone of
Durham at Byers’ Quarry, where it is a rare fossil.

4, Cyrwere (Cyrueripets) Jonsstana, Kirkby, Ann. & Mag. Nat.
Hist., ser. 3. vol. ii. p. 432, pl. 11. figs. 1, 2; and Trans. Tyne.
Nat. Field-club, vol. iv. p. 151, pl. 11. figs. 24, 25.

Syn. Bairdia gracilis, Reuss (not McCoy).

Occurs rarely at Hampole.

5. Krexpya Permrana, Jones, Monog. Perm. Foss. of England, p. 66.
pl. 18. fig. 1; and Trans. Tyne. Nat. Field-club, vol. iv. p. 129,
pl. 8 a. figs. 1-9.

I have only met with this species once at Hampole. The specimen
found agrees in size and general character with those of the Shell-
limestone of Durham ; the sculpture of the valves is well marked.

The specimens of Entomestraca which I have obtained at Hampole
are pretty well preserved, and are generally perfect carapaces*. One
of the beds at this locality is very friable, and decays rapidly by the
action of the weather ; and it is in the débris thus formed that I have
found most of my Yorkshire examples of this class.

ForAMINIFERA.

1. Mirroza pusiiza, Geinitz, Sp. Verstein. Zechstein. und Roth.,
p. 6, pl. 3. figs. 3-6.
Rather common at Hampole along with the Entomostraca. In

* The locality of Hampole is so often mentioned in this memoir, and is so well
worthy of further search, that I may remark that it refers to a little old quarry
by the side of the road leading from Doncaster to Wakefield, a short distance to
the west of the village, and not far from the Swan Inn.

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE, 309

most cases oval-shaped and flat; the coils approximating more
or less to a regular arrangement on one plane, as in Spirillina.
Rarely disk-shaped, simulating (?) the Spirillina. Occasionally
more globose or cylindrical in form,—the coils overlapping irre-
gularly, as generally occurs in Durham examples. The coils are also
narrower, and the general habit of the specimens less robust than
in Durham examples.

Usual size: 54th in. long, jth in. greatest width, 4, in. least
width ; largest specimens, ;4,th in. long, jth in. greatest width,
qgth in. least width.

In Yorkshire it only occurs at Hampole. It is not rare in the
Shell-limestone of Durham, nor in the Unter Zechstein of Germany.

ALG,

The surfaces of slabs in the Brotherton Beds are often covered with
the remains of an obscure fossil which probably belongs to the Alge.
The fragments are filiform, linear or slightly curved, cylindrical or
rather compressed, rarely branched, about an inch in length when
longest, but generally shorter, and about j4,th of an inch or less in
breadth. They are often of a brown or reddish tinge—the surface
of the slabs being grey or yellowish—and stand out in relief. They
show no trace of structure; and they not only occur on the surface
of the slabs, but in the substance of the beds.

These are often associated with Awinus dubius. At Knottingley
the fragments are arranged linearly, with their longer axis in one
direction, as if by the influence of a current. Indeed the imperfect
condition of the specimens, and the manner in which they are
scattered over the surface of the slabs, would seem to indicate that
they were all more or less subjected to drift-action.

In the Upper Limestone of Durham—the equivalent of the
Brotherton Beds—obscure remains of Alge similar to those under
notice likewise occur, and they are also associated with the same
shell. These remains are in a carbonized state, and are scarcely so
much broken up as those of Yorkshire, but they possess much the
same character as the latter, and it is not improbable that they may
belong to the same species.

The obscure fossils resembling Serpula or Dentalium, noticed by
Prof. Sedgwick in the Brotherton Beds at Cold Hill, near Aberford*,
are probably identical with this fossil.

Loc. In Brotherton Beds at Knottingley, Pickburn Leys, and
Wadworth.

The occurrence of another fossil, of somewhat obscure affinities,
though possibly an Annelid, may here be noticed.

It is a cast of a laterally compressed tube, 3 inches long (neither end
being perfect), 2ths of an inch in longest width, and. ths in shorter
width. It is slightly arcuate longitudinally, and has an oval, or
rather ovate section transyersely—the convex edge being more
flatly rounded than the other. Between the cast and the investing
matrix there is a slight space, which appears to have been originally
occupied by the walls of the tube.

* Trans. Geol. Soc., 2nd ser. vol. i. p. 118.

310 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

A similar fossil has occurred in the Shell- and Compact; Limestones
of Durham, agreeing in most respects with the one described.

Loc. In Lower Limestone at Hampole Stubbs, and from a
roadside stone-heap between Hampole and Hooton Pagnell.

The following table gives a synoptical view of the Permian species
of South Yorkshire, and shows their general distribution in the
Permian deposits of Britain :—

South Yorkshire. Durham.
3 :
. g ae § él al eile
Names of Genus, Species, &e. Meese es ell lacs g| €| S| S38
Ss) 3/2. (F/Sis| | 21s] ssiee
S/S) 32 | 8/3] 51813) s} SB) Si Ps
tm) 5) BS] S| A]! eof Sl] eB) 8] 4] 2) ns :
Sn) Ps | 8) si]. 2)a] s/ 4] al silica iis
= SSS Sle slalgslalgizels
6 8) 89 | 2) 5) 318) 8) 8) a Sie a iis
Bi\Ala |Rlalielslol nO alae |e
1 |x NautilusFreieslebeni, Geinitz od} t5 |) 685 ido) dcell aeellans x | #
2 |* Turbo helicinus, Schloth. (31 (eeere bee Aa | bxad ancl ee ea a ee |
3 | Rissoa Leighi, Brown ...... Scq||@21) S08. |} c6)oneHl kel boq}{soq|loae|[ocel]o00 x lx
4 | Turritella Altenburgensis, |
Geinitz aesesccstee ces nog) Se|| 006. \looo|)ooelloacl|ooc % [ede *
5 | Chemnitzia Roesleri, Geinitz.|...)*| ... |...}...||...[..- | ¥
6 | Straparollus Permianus, |
; ORG Van See Asie saliesaaens Sad eel Ado. |oo8| bal Hood) [bos .| *
7 | Natica minima? Brown GA 36: lesan cel eae ITs al ee el eee eae *
8 |x Chiton Loftusianus, King...|...|*| ... |...[..- .|
9 |x Dentalium Sorbyi, King Poy Selec alana eek 1. |
10 |x Monotis speluncaria, Schloth.|.. | x x | *
I] |x Gervillia antiqua, Miins?. ... Le * | * |. x lls
12 |x keratophaga, Schloth. |...| «| seals | %
13 |x Myalina Hausmanni, Goldf. |...) x | * *]...[ 3] * woe HBG
14 | Myoconcha costata, Brown. |...) *| ... |...[..[)...[..- w]e] ft] xe |e
15 |x Macrodon striatus, Schloth. |...)%| ... |...}...|[..[.. wo .|
16 Leda spelunearia, Geinitz...|... Fail dee || foo5| hoe||/seq}loce|| fe |laa}e3
17 |x Axinus dubius, Sch/oth. var.) | |
obscurus, Sow.” :.......---- seeloent * % | * | % * 1%
; , new variety...) ¥ |
18 | Cardiomorpha Pallasi, De
Varies sth haha sae tocdecee lee [| #
19 |x Terebratulaelongata, Schloth|.. | x | | * | |
20 | Acanthocladiaanceps, Sch/oth|...| * * | x |
21 Thamniscus dubius, Schloth.|... A aaa eS) hac le Bale *
22 | Retepora Ehrenbergi, Geinitz|...)*| ... |...|... |. | % | *
23 | StenoporaMackrothi, Geinitz|...|*| ... |...J... Bee Bea ones Bedioncil| cis |||
24} Cythere (Bairdia) plebeia, | | |
RUSS Raat Ee ee saahte| || * | %
25 | —— -—— Schaurothiana,| |
DG ALI ReBerpacncbe nr ecRooeee Bag ea aha. BRdl Bel | petal Paeltoaed be |
26 | —— ampla, Reuss. ...)...|%| ... |e.-[es-|[..-[---[---[eo] |
27 | ——(Cytherideis)Jonesiana,| |
Kar hby yosesececee near aealldes sae: lasa|sce|leocl eeleres exer oe
28 | Kirkbya Permiana, Jones ...|....% |... |..J...|]..J..-f...} |
29 | Miliola pusilla, Geinite...... veo] % ese boe * | % |. . | *
30 |x?Sp. undetermined (Alga) ...|...)... Milt | Seal eee *
31 | Sp. undetermined (Tubular |
fossil) (eee, a2) 2. eee eee Oye esac ee eee | allies x | %
Pe i Ved a

1861. | KIRKBY—PERMIAN, SOUTH YORKSHIRE. 311

Those species with asterisks on their left have been previously
noticed by Professors Phillips, Sedgwick, and King, as occurring in
Yorkshire.

It is stated by Prof.Sedgwick that Productus horridus (or P.calvus)
was found by him in the “upper thin-bedded limestone” between
Nosterfield and Well*. It is very difficult to doubt the observation
of Prof. Sedgwick; but I can scarcely help doing so in the present
instance when I consider the utter absence of Brachiopods in all the
Upper Permian Beds, not only of England, but of Western Europe
generally.

§ V. Distribution of the Fossils.—This list of fossils contains all
that are yet known to occur in the Permian rocks of South Yorkshire.
Without including the localities searched by Profs. Sedgwick and
Phillips, it represents the result of an examination of not less than
twenty fossiliferous localities visited by myself. If we add to these
the localities examined by the geologists named, and not visited by
me, and consider that they only met with one species which I have
not found, I think we may almost conclude that the list given takes
in most, if not all, of the common fossils of the district. Nevertheless
it is not to be doubted that a more continued search would add to the
number of species, and improve our knowledge of them generally.

It will be apparent enough from this list that fossils are only found
in two subdivisions—in the Lower Limestone and the Brotherton
Beds. And it will be just as apparent that nearly all the species
are confined to the Lower Limestone, only three occurring in the
Brotherton Beds. What we know, therefore, of the fossils of the
Permian rocks of this district is in the main derived from a single
subdivision belonging to the inferior half of the series.

A. Fossils of the Lower Limestone.—In the Lower Limestone the
best localities for fossils are in the oolitic, and what I have termed the
polyzoan beds. Fossils are found throughout the whole of the various
beds of this member, but are most plentiful, both in species and
individuals, in the beds mentioned. They are not, however, well
preserved, being in most cases casts merely, those of Hampole being
the chief exception. The best localities—those most rich in species
and individuals, and where the latter are most finely developed and
best preserved—that I had the opportunity of examining are the old
quarries at Hampole, Hampole Stubbs, and Moorhouse, the Free-
stone Quarry near Brodsworth, and the Holywell Hill Quarries at
Conisborough; all of which would certainly repay further examination,
and particularly the continued researches of a local geologist. In all
localities the Conchifera are generally found in single valves. This
holds good with every species of this classt. The Polyzoa too are

* Trans. Geol. Soc., 2nd ser. vol. iii. p. 108.

+ The dislocation of the valves of fossil Conchifera does not necessarily imply
that they were subjected to the action of currents, and probably transported from
distant regions prior to their being imbedded in sediment and fossilized. In
most cases when a Conchifer dies and its adductor muscles relax, the valves of its
shell spring open more or less by the elasticity of the ligament. And should the
valves thus remain for a moderate length of time uncovered by sediment, the
ligament and fleshy portion of the Mollusk decay, or are otherwise removed, and

312 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

always more or less fragmentary. The Gasteropoda seem to have
suffered no injury prior to inhumation. In several places the spe-
cimens, even as casts, are so badly preserved as scarcely to be
determinable. ‘This appears to result from two causes,—sometimes
being apparently the fault of the investing matrix, whose preservative
qualities have been poor; and at others it is owing to the distortion
of the specimens by compression during the process of fossilization.
The most remarkable instance of the latter kind that I have met
with is near to Hampole Stubbs, where there is a bed of compact
brown limestone full of Aaini pressed flat, and, in consequence,
broken into many pieces. I observed another example of this kind
at Conisborough, where Terebratula elongata, which is not a rare
shell there, and of rather large size for Yorkshire, is almost invariably
more or less distorted by pressure, while the shells of other species—
Gasteropods and Conchifers—are scarcely ever similarly affected. In
this case the Terebratule must have been less able to resist the amount
of pressure to which the organic remains of this locality were sub-
jected than their associates. And perhaps this may be explained, in
the first place, by their much thinner shell, and in the second, because
of their having been imbedded with closed valves, their dental system
notallowing the easy opening or dislocation of thevalves after thedeath
of the Mollusk, which would thus prevent the entrance of sediment into
the cavity of the shell, to the great disadvantage of the valves resisting
the pressure of the gradually increasing superincumbent mass.

Moorhouse.—One of the most interesting localities is an old quarry
near to the hamlet of Moorhouse, where Aainus dubius occurs in
great profusion, and most finely developed, both in respect to size,
thickness of shell, and general character. Its peculiar umbonal
ridges are very finely displayed in the casts of this locality. Several
other species hkewise occur, and amongst them some of the rarest
of the Yorkshire forms. ‘The limestone is oolitic; and there is one
bed in particular which contains the fossils most abundantly ; its
position is only seven or eight feet above the Lower Red Sandstone,
which is exposed in the same quarry.

Hampole.—About half a mile to the east of the preceding locality
is another old quarry, of very ignoble appearance, at Hampole, where
there are some beds of fossiliferous limestone apparently situated a
little above the oolitic beds of Moorhouse. From this spot I have
obtained seventeen species, and many of them are immature and some-
what dwarfed. Awinus dubius, which is so large at Moorhouse, is here
never more than half-an-inch in width. And Turbo helicinus, which

all connexion between the valves ceases, in which state they would subsequently
be imbedded, were a deposition of sediment to take place before the decay of the
valves themselves. It is extremely probable that this is one of the causes of the
valves of fossil Conchifera so often occurring detached. When shells of this
class are found fossilized with their valves closed and in perfect juxtaposition, it
is natural to suppose that their ligament was slight and of little strength, or that
they were burrowers, or, at least, if not burrowers, that they had been enveloped
in sediment while living; so that, on the relaxation of the adductor muscles from
death, the valves would be kept closed by the external pressure of the surrounding
sediment.

1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 313

is the common fossil of the locality, is only one-fourth its usual size.
The molluscan remains are mixed with comminuted Polyzoa, chiefly
of the species Acan. anceps, the fragments being very small, though
numerous. As it happens, however, the reduction in size of the
fossils is accompanied by an improvement in their state of preserva-
tion, and particularly in respect to the Univalves, which are generally
testiferous. So numerous are these minute fossils in some parts of the
quarry, that the quantity of them that occur in a small portion of
matrix is most surprising, a fact rendered easy of proof by the
friable nature of the matrix. As illustrative of this, | may mention
that in but a quarter of an ounce of limestone I have picked out
298 separate organisms, the majority being specimens of Turbo hel-
cinus. Another experiment of a like kind, the quantity of limestone
being the same, yielded even more astonishing results. From it I
extracted 461 specimens of 7. helicenus, 18 of Turrit. Altenburgensis,
7 of Ris. Leight, 2 of Terebrat. elongata, 1 of Bairdia plebeia, 24 of
Miliola pusilla, and 8 fragments of Stenopora Mackrothi; in all 513
organisms. A cubic foot of this limestone of equal richness as the
latter throughout, and supposing it to weigh 120 lbs. (a low estimate),
would contain very nearly 4,000,000 of distinct individuals—
and these not truly microscopic, but distinguishable with the naked
eye, most of them being Gasteropodous Mollusea. All the limestone
of this locality, however, is not so highly fossiliferous as in these
examples, there apparently being certain zones of limestone that are
pre-eminently fossiliferous. Besides illustrating the extreme abun-
dance of these minute fossils, the above facts give a good idea of the
relative abundance of individuals belonging to the different species.
They show that Turbo helicinus is by far the most common form, and
that its individuals outnumber many times over the aggregate of those
of all the other species. And this is the only instance I have met with
where the Gasteropod in question, though very generally distributed
in the Lower Limestone, has taken the leading place among the fossils
of a locality. And, besides, this is the only locality in Yorkshire-—per-
haps in England—where G'asteropoda hold so important a position in
the list of species, about half of the Mollusca being species of this class.
Near Brodsworth.—Another interesting locality is near to Brods-
worth in some old quarries just to the west of the village, where the
beds belong to the higher part of the Lower Limestone. The pre-
dominating fossil here is Gervillia antiqua, its casts composing almost
the whole of the substance of some of the beds. This species is just
as common here as Awinus dubius is at Moorhouse, or Turbo helicinus
at Hampole. And the beds in which it is so plentiful are probably
identical with those at Wentbridge, Pontefract, etc., where we have
noticed it as occurring in similar profusion. Along with the Gervil-
he are to be found the remains of a few other species, amongst which
(rarely) are those of Nautilus Freveslebeni and Chiton Loftusianus.
Near Pickburn.—Between Pickburn and Marr there is a quarry
called by the villagers the “‘ Freestone Quarry * ”—of thick-bedded

* In the south of Yorkshire any stone that can be easily worked by the mason
is termed a “freestone.” In Durham this term is only applied to sandstones.

314 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

oolitic and polyzoan limestone, from which I obtained an interesting
suite of fossils. The common fossil is a Polyzoon—Acanthocladia
anceps. The associated species, among which are those mentioned as
the common fossils of other localities,are all of subordinate importance
in respect to individual distribution. Besides the species of Polyzoa
named, three others have occurred to me in the polyzoan beds, two of
which (Retepora Ehrenbergi and Thamniscus dubius) are peculiar to
it. The beds in which the Polyzoa are so profusely distributed
scarcely ever contain species belonging to other classes.

I chiefly notice these fossiliferous localities in detail to draw some
attention to the manner in which different species characterize certain
localities. In some cases this seems to be due to the localities repre-
senting different horizons of the Lower Limestone, consequently difter-
ent periods of Permian time, which in this area were characterized
by the prevalence of different common species. This is certainly
the case with the Moorhouse and Brodsworth localities, whose
vertical position in the series it 1s not difficult to test, the former
evidently underlying the latter. In other instances the differences
observed appear to be merely those of geographical distribution ;
as, for example, that of Hampole and the Freestone Quarry
near Pickburn, the beds of both appearing to be of the same relative
position. ‘To the paleontologist these groups of species and their
differences are of particular importance—just as much, perhaps, as
the larger groups (and their differences) belonging to different
formations of strata: for, as the one tells of great and wide-
spread changes in the relations of ancient lfe during the elapse of
immense ages, so does the other of the small and limited changes
which happened during shorter periods, and from which the first
eventuate.

The species that are found furthest down im the Lower Limestone
are Awvinus dubius and Gervillia antiqua. Casts of these shells
(those of the former being most prevalent) occur in the lowest beds of
compact and earthy limestones immediately above the Rothhegendes
at Carlton, Wentbridge, and Pontefract (Bagg Hill). Other species
soon appear in the beds that follow; but for some feet upwards
Axinus dubius holds its own, and increases in size and numbers,
until it attains its maximum in certain strata, not so very far above
the sandstone as at Moorhouse and Conisborough. In the succeeding
beds Gervillia antiqua becomes very numerous and takes the place of
the other as common species. Near about the same horizon as the
latter, or possibly a little below it, are the beds in which Acanthocladia
anceps is so common in the region between the Don and the Went.
Above these beds and in the highest portion of the member, fossils
become rarer, and the species that occur are more equally represented.

The assemblage of fossils at Hampole is, perhaps, the most curious
of any that occurred to me in South Yorkshire. As already remarked,
it is chiefly composed of Univalves, all of which are minute, their
small size being due in the case of Turbo helicinus, Turritella Alten-
burgensis, and one or two others, to the immature condition of the
specimens, which are invariably young and somewhat dwarfed

1861. | KIRKBY—PERMIAN, SOUTH YORKSHIRE, 315

individuals, The associated specimens of Rissoa Leight, Natica
minima, and Straparollus Permianus are mature individuals, so far
as the development of these species is known to us from their occur-
rence in the Permian strata of other districts. The latter, however,
are smaller species than the former, and their individuals are of
about similar gravities as the immature examples of the first-named
species. Hence when we consider their great numbers, smallness, and
general uniformity of size, and the comminuted state of the Polyzoa
that occur along with them, it seems likely that we have here an
instance of the accumulating action of currents. It is easy to
understand how a submarine current of a certain power, passing over
a sea-bottom strewed with various forms of marine life, could sweep
away those organisms whose specific gravities it could overcome to
some region more or less distant, where its force became spent or
lessened, and there deposit them in quantities as countless as those of
Hampole. If its power never excceded a certain limit, the larger and
more weighty organisms would not be removed, while the smaller, if
unattached and not otherwise held down, would be earried off; and
supposing the currents were periodical and occurring only at stated
seasons, hosts of young shells at a particular stage of development
might be swept away at intervals. It must certainly be allowed
that the fossils individually show no perceptible traces of such a
removal, though to what extent traces of this kind in the shape of
abrasion, etc., would be perceptible in the case of transportation over
a soft sea-bottom, such as the Lower Limestone in the course of
deposition would surely form, does not appear, though we can readily
conceive that they would possibly not be very evident. There may
be other ways of accounting for the aggregation of so many minute
Univalves in one locality ; but I certainly know of none that so well
explains the facts of the case as the one suggested. Nor do I know
of any other instance in the Permian deposits of Yorkshire and
Durham, where we seem to have such indications of the influence of
ancient submarine currents in the distribution or rather accumulation
of their organic remains.

The polyzoan beds also seem to be at first sight an accumulation of
drifted materials. This is only a natural surmise on finding so
fragmentary an assemblage of remains as those which enter so largely
into the composition of these strata. Nevertheless I am disposed to
consider them the remains of Polyzoa that lived where we find them,
and that the range of the beds marks the site of an ancient ground
or zone altogether (or nearly so) peopled by Polyzoa,—where they
lived and died generation after generation for a long period, the latter
generations growing on a sea-bottom composed of fragments of the
polypidoms that preceded them, until at last, owing toreasonsunknown,
their growth ceased after the accumulation of several thick beds of
their remains. This I think is proved by the fossils belonging nearly
altogether to Polyzoa. Had they been accumulated by the action of
a current sweeping over the bottom of the sea, there would surely
be observed amongst them a greater mixture of other species, more
especially as we know that there were several others which helped

316 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

to people the sea-bottom of the South Yorkshire region during the
aggregation of the beds,

B. Fossils of the Brotherton Beds.—Little can be said relative to
any peculiarities in the distribution of fossils in the Brotherton Beds.
The chief feature is most certainly their great paucity both specifi-
cally and individually. The three species which occur in them are
generally associated ; when any one of them is found alone, it is
Awinus dubius. Their occurrence is not general throughout the
vertical thickness of the beds, there being many of the strata quite
unfossiliferous. They characterize certain strata, and on the upper
surfaces of these they are often rather thickly strewed. The
size of the two Conchifers which occur is greatly reduced in the
Brotherton Beds, more particularly in the case of Aw. dubius. Here
it never exceeds half-an-inch in width, while in the Lower Lime-
stone it is at times fully two inches. It also shows slight modifica-
tions of form, approaching in outline the variety Schlotheime of
Geinitz, though somewhat intermediate between it and obscurus.
The only species peculiar to these beds is the Alga already noticed.

§ VL. Permian Fossils of South Yorkshire compared with those
of Durham.—An examination of the preceding table shows that all
the species, with the exception of two, occur in the Permian beds of
Durham ; and both of these are found in the Lancashire beds. It is
thus seen that none are peculiar to South Yorkshire. It is also
evident that most of the species are not confined to the British area,
several being among the most sporadic of Permian species. Out of
the 31 species 25 are common to Germany and Britain, most of
which existed in the former region at the period of the Lower Lime-
stone. ‘Ten species are common to Russia and Germany, and a less
number (4) to Russia, Germany, and the Permian strata of North
America. The Conchifera, along with the Cephalopod and the Bra-
chiopod, are all extra-British ; two-thirds of the former and each
of the representatives of the latter classes range through Germany
into Russia. All the Polyzoa are German; but none are Russian.
The Entomostraca, with one exception (Bairdia Schaurothiana), are
German, one (Kirkbya Permiana) having also Russian varieties.
The Rhizopod is a Zechstein ‘species. The species most confined in
their range are Gasteropods. Of the members of this class only one
is Russian, 5 are German, and 3 are peculiar to Britain. In all,
© species appear to be confined to the British area.

Compared with the Permian fauna of Durham—taking it at its
maximum development during the deposition of the Shell-limestone
—the group of species found in the Lower Limestone forms but a
meagre life-group so far as number of species is concerned. The
number of species composing the former is 118, while of the latter
there are only 31. This does not, however, prove a rarity of life in
the Yorkshire area; for the fewness of species seems to haye been
counterbalanced in some degree by a greater individual abundance,
—the remains of Gervillie at Wentbridge, &c., and of Turbo helicinus
at Hampole, exceeding anything of the kind to be observed in the
most fossiliferous localities of Durham. The chief differences are

laf

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE. 31%

absences, that of Brachiopoda being the most notable. In the most fos-
siliferous localities in Durham, Brachiopods are the commonest fossils.
In Yorkshire the only species of this class that occurs is almost among
the rarest. The twocommon Polyzoans of Durham—Fenestella reti-
formis and Synocladia virgulacea—are also wanting, their places being
apparently taken by Acanthocladia anceps. The commonKchinoderm
of Durham is absent, as are also other species too numerous to name,
several of which are common forms in the Durham beds. On the other
hand, Nautilus Freieslebent, Chemnitzia Roessleri, Straparollus Per-
muanus, Chiton Loftusianus, Monotis speluncaria, Macrodon striatus,
Terebratula elongata, Acanthocladia anceps, Retepora Ehrenberg,
Miliola pusilla, as well as others that are common to both faunze, and
which in Durham and Germany are confined to the lower and middle
subdivisions, form a most intimate relationship between the two, and
afford strong paleontological evidence—were any wanting—of the
inferior position in the series of the deposits containing the Yorkshire
group of species.

But to form a just comparison with the Durham fauna, we must
take it as developed during the deposition of the Compact Limestone,
the equivalent—in great measure—of the Lower Limestone. But
before doing this, it may again be pointed out that the fossils of the
Compact Limestone do not represent the earliest traces of Permian
life in Durham, as do those of the Lower Limestone in Yorkshire.
In the latter county the deposition of the Lower Red Sandstone or
Rothliegendes was immediately followed by that of the Lower Lime-
stone ; at least there was no intermediate deposition. In Durhama
deposit of semicalcareous, semiargillaceous sediment followed that
of the Rothliegendes, and preceded that of the Compact Limestone
—thus separating the two deposits by a few feet of calcareous shale,
which has been named the Marl-slate. It was during the deposi-
tion of this shale that animal life may be said to have first appeared
in the Durham area during Permian time,—Lingula Credneri, Dis-
cina Konincki, and Myalina Hausmanm, with several Fishes, forming
this avant-garde of the larger fauna that afterwards peopled the
same area. I have little doubt that these species were contempora-
ries with those of the fauna of the Lower Limestone, though only for
a season; for on the commencement of deposition of the Compact
Limestone, another set of species gradually took their place, and be-
came in turn contemporaries of the same Yorkshire species, which
continued to people the Yorkshire area while the changes noticed
were occurring in Durham. And it was not until the era of the
Compact Limestone that the physical conditions of the Durham area
became analogous to those prevailing in the area of Yorkshire, and
that the distribution of species therein became, like those of York-
shire, of an unquestionably marine character. It is, therefore,
chiefly with them that we have to do in comparing the contem-
porary faunze of the two districts.

As far as we are acquainted with the fossils of the Compact Lime-
stone, they amount to 31 species, thus forming a group of equal num-
ber with those of the Lower Limestone. A list of these species is

318 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,
given in the following table, the Mollusca and Polyzoa of the Lower
Limestone being placed in juxtaposition for the sake of easy
comparison :—

Compact Limestone (Durham). Lower Limestone (South York-

re )*
Dentalina Permiana. shire)*.
Miliola pusilla.
Kirkbya Permiana. * K. Permiana.

Retepora Ehrenbergi.
Acanthocladia anceps.
Fenestella retiformis.

x Retepora Ehrenbergi.
x Acanthocladia anceps.

Stenopora Mackrothi, * Stenopora Mackrothi.
Synocladia virgulacea.

Thamniscus dubius.
Lingula Credneri.

Discina Konincki.
Productus horridus.
Strophalosia lamellosa.

— Goldfussi.
Streptorhynchus pelargonatus.
Spirifera alata.

Camarophoria crumena.
globulina.
Spirifera Urii.

Terebratula elongata.
Monotis speluncaria.
Gervillia antiqua.

Axinus dubius.
Myoconcha costata.
Leda speluncaria.
Astarte Vallisnieriana.
Tunstallensis.
Solemya biarmica.
normalis.
Pecten pusillus.
Myacites lunulata.

Pleurotomaria Verneuili.

Nautilus Freieslebeni.
+ Platysomus striatus.

* Terebratula elongata.
x Monotis speluncaria.
* Gervillia antiqua.

* ———— keratophaga.
~ Axinus dubius.

x Myoconcha costata.

x Leda speluncaria.

Myalina Hausmanni.
x Cardiomorpha Pallasi.
«x Macrodon striatus.

Turbo helicinus.
Rissoa Leighi.
Turrit. Altenburgensis.
¥ Chemnitzia Roessleri.
Natica minima.
Chiton Loftusianus.
* Dentalium Sorbyi.
x Straparollus Permianus.
x Nautilus Freieslebeni.

It is thus seen that 11 species are common to both groups,
amongst which are the Cephalopod, 5 Conchifers, the Brachiopod,
3 Polyzoans, and 1 Entomostracan. When we consider the nearness
of the two areas—their distance apart being only about 80 miles—

* The species marked with asterisks occur in the Zechstein.
t The list of species from the Compact Limestone is based upon the researches
of Prof. King, Mr. Howse, Mr. Manson, and Mr. Parker.

1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRE. ol9

so slight an admixture of species is a matter of surprise, particu-
larly when an examination of the fauna of the Unter Zechstein,
which appears to have been of contemporaneous deposition with the
Compact Limestone of Durham and the Lower Limestone of York-
shire, shows that 21 of the Yorkshire species (viz. 1 Cephalopod,
3 Gasteropods, 8 Conchifers, 1 Brachiopod, 3 Polyzoans, 4 Entomostra-
eans, and 1 Rhizopod) were distributed in the German area during
the same period.

In the Yorkshire fauna 9 of the species are Gasteropods ; in that
of the Compact Limestone there is only a single member of the same
class. In the Compact Limestone fauna 11 of the species are Bra-
chiopods; in the other there is only one. It is in these respects
that the two faunee differ most. Five out of the 9 Yorkshire Conchifera
occur in the Compact Limestone: among them are the two common
species Aw. dubius and Gerv. antiqua; but neither of these shells
is common there. The most common shell of the Compact Limestone
is Productus horridus. No species is so common as it; Strophalosia
lamellosa, Spirifera alata, and Camarophoria crumena being next in
the list of common species. Acanthocladia anceps, the common Poly-
zoan of the Lower Limestone, is not rare in the Compact Limestone,
but the place of the common Polyzoan is there taken by Fenestella
retiformis. One of the Yorkshire Entomostraca is found in the
Durham subdivision. The Rhizopod Miliola pusilla is common to
both faunee, it being accompanied by a Dentalina in the Compact
Limestone.

In these differences, in two contemporaneous assemblages of Per-
mian species, we have a good illustration of some of the peculiarities
that pertained to the distribution of marine life in paleeozoic times.
It is thus shown that, according to present researches, there is only
about one-third of the species of each fauna common to both groups,
thus leaving about two-thirds that are peculiar to each. And it
may be remarked that, though all the species peculiar to the South
Yorkshire assemblage, except two, were afterwards distributed in
the Durham area during the Shell-limestone period, it would yet
appear that none of those peculiar to the Durham group were ever
common to the other. We can scarcely refer these differences
to the result of geographical distribution of species, for we cannot
but consider that the Permian deposits of Durham and Yorkshire
were accumulated in the same sea; so that it would be perfectly
unwarrantable to ascribe differences so great in specific distribu-
tion to an agency of this kind, when the two regions were so
nearly situated and the nature of the sea-bottom the same. To
changes belonging to the distribution of species in depth, however,
the differences would easily seem referable; it being now well
known that great differences obtain in the distribution of marine
life as the zone of depth varies, even with short distances. I would
therefore refer the differences observed in these local faune to a
change in the conditions of depth of sea existing in each area, while
their respective deposits were accumulating; the difference being in
the greater depth of sea over the Durham area than to the south-

VOL. XVII.—PART I. Z

320 PROCEEDINGS OF THE GEOLOGICAL SOCYETY. [Mar. 6,

ward over the other. It is probable when we acquire a better
~ knowledge of the fossils occurring in the intervening range of
Permian strata in the northern half of Yorkshire, that the differ-
ences noticed may be found to be the result of gradual changes in
the distribution of species. And it is possible that still further
south other arrangements of species may obtain that are peculiar to
their own localities; just as in the case of the two following local
faunze which, in all probability, had a contemporaneous existence
further to the west.

It is worthy of attention that several of the Yorkshire species,
which were of contemporaneous existence in Germany, appeared in
the British area first in Yorkshire. This is the case with Chemnitzia
Roessleri, Dentalium Sorbyi, Turbo helicinus, Straparollus Permianus,
Turritella Altenburgensis, and Macrodon striatus, which did not ap-
pear in the Durham area until the era of the Shell-limestone. It is
not very evident whether in the latter case the migration was from
the Yorkshire region or that of Germany; but as other species ac-
companied these which do not occur in the Lower Limestone of York-
shire, though common to the Unter Zechstein, it may be presumed
that it proceeded from the latter. Indeed, when we remember that
the Permian fauna attained its maximum in Germany during the
period of the Unter Zechstein*, and in England not until that of the
Shell-limestone, it seems highly probable that a general migration
of species—or rather of their individuals, the species still continuing
in the old area—took place to the westward while the middle portion
of the Permian series was being deposited, especially as more than
half of the additions to the British fauna during the Shell-limestone
period were Unter Zechstein species.

§ VIL. Permian Fossils of South Yorkshire compared with those
of Lancashire.—There is another group of species with which it may
be well to institute a comparison. I refer to that belonging to the
Permian strata of Lancashire, whose geographical position is nearer to
the Yorkshire beds than that of the Compact Limestone, though
their vertical position in the series is not so well determined. This
little local fauna consists of only seven species ; three of these are
Gasteropods—viz. Turbo helicinus (with var. Mancuniensis), Rissoa
Leight (with var. Gibsoni), and Natica minima. The rest, with the
exception of a Sponge(Zragos Binney?), are Conchifers—viz. Gervillia
antiqua, Aainus dubius, and Myoconcha costata. Now all these
species, except the Sponge, occur in Yorkshire; and all of them are
common species there, but the one just-named and Natica minima.
Two of the species we readily recognize as the most common of the
Yorkshire fauna. And two of the Univalves (Natica minima and
Rissoa Leighi) are in England only found in the Lancashire and
Yorkshire beds.

Therefore making every allowance forthesmallnessof the Lancashire
group of species, there seems to be a much more intimate relation-
ship between it and the Yorkshire fauna (Lower Limestone), than

* See an excellent table of species occurring in the Zechstein of Germany, by
Baron von Schauroth, in the Zeitsch. d. Deut. geol. Gesell. 1854, pp. 569, 574.

1861. ] KIRKBY—PERMIAN, SOUTH YORKSHIRN. 321

between the latter and the Durham fauna during the Compact Lime-
stone era. It is certainly difficult to attempt comparisons with so
small a group of species, which may or may not give a fair idea of
the original distribution of life in that area, though I incline to the
former opinion. We see, however, the same ascendency of Gastero-
pods and Conchifers, and the same rarity of Brachiopods that obtain in
the fauna of the Lower Limestone of Yorkshire. And in these respects
we might almost argue a similarity of physical conditions prevailing
in the two areas. But the absence of Polyzoa and the great reduc-
tion in the number of species point to a difference as great perhaps
as that which existed between the conditions of the Yorkshire and
Durham areas. Between the Lancashire and the Durham faune, that
of Yorkshire holds an intermediate place. Its zone of depth, as
already remarked, was apparently not so great as that of the Compact
Limestone, though decidedly greater than that of the sea of the Lan-
cashire area. The fauna of the latter appears to have existed on the
argillaceous and semicalcareous submarine mud-flats that lay off the
coast of a Permian land-area ; the Yorkshire fauna certainly existed
further away in deeper water and within the limits of regular depo-
sition of caleareous sediment, though still towards the shallower
zones of that region ; the fauna of the Compact Limestone of Dur-
ham seems to have dwelt still further seaward, where the depth was
greatest. These conclusions are in perfect harmony with the teach-
ings of a more comprehensive view of the Permian deposits of Bri-
tain; for an examination of them leads to the opinion that the sea
which covered so much of the British area in Permian times, deepened
to the north and east and shallowed to the south and west. This we
may easily prove by tracing the Permian strata from the north-east
corner of Durham south and westward, noting the gradual change
from magnesian-calcareous deposits to others which are argillaceous,
arenaceous, and conglomeratic,—these lithological changes being
likewise accompanied by analogous changes in the distribution of
the remains of organic life, there being at the one extreme (Durham)
a deep-sea fauna in calcareous strata, and at the other (Bristol) a
conglomerate charged with the remains of Reptiles.

As before stated, the exact horizon of the fossiliferous beds of the
Lancashire series has not been determined; nor is it easy to do so.
But it may be suggested that, as the beds in question (which are thin
limestones and marls) most probably represent the period of greatest
depth of sea attained in the Lancashire area in Permian time, being
the only calcareous beds of the series, they may easily be of synchro-
nous deposition with the Lower and Compact Limestones, which are
considered to be representatives of the same period in their respective
areas. This would certainly be the case if the depression of sea-bot-
tom, which originated the increased depth of sea, arrived at its maxi-
mum in all parts of the British area at the same time: and, so far
as we know, there is nothing that seems to disprove that it did; at
least it is much more likely, when we consider the nearness of the
Lancashire and Yorkshire areas, that they were affected alike and
attained their maximum depth of sea about the same time, than that

Zz 2

322 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 6,

they were affected differently and attained their maximum depths
at widely different periods *. Granting the former, the comparison
we have instituted with the Lancashire fauna is attended with some
degree of interest ; for it then relates to a group of species of contem-
poraneous existence with that of the Lower Limestone, as in the case
of the Compact-limestone group.

I am aware that Prof. King has incidentally suggested that these
beds may possibly belong to the highest portion of the Permian
series. But, except the weight of his opimion (for which I make
every allowance), I see no fact that supports such a view. And
besides the argument already offered in favour of a different classi-
fication, there is the fact that four of the species (G. antiqua, R. Leight,
N. minima, and T. Binney) never occur in the higher beds of the
Permian series in other parts of England. This might not be of
much consequence were the distribution of species at all variable in
the upper beds, so that we might expect to meet with species spe-
cially characteristic of certain localities; but there is so great a
uniformity of distribution in the highest beds of the series—the very
reverse of that in the lowest—that the occurrence of species hitherto
found only in the inferior strata in beds of uncertain horizons would
certainly favour their classification with the lower rather than the
upper members of the series.

§ VILL. Permian Fossilsof Ireland.—Butthe group of Permian species
to which the fauna of the Lower Limestone approaches most closely is
that occurring in the magnesian limestone of Cultra and Tullyconnell
in Ireland, described by Prof. Kingt. This group consists of 11
species; and all of them with one exception (Cythere Tyronica) are
common to the Yorkshire fauna. Among the Mollusca are the com-
mon forms of the Yorkshire deposit, as Gerv. antiqua, Aw. dubius, Myo.
costata, Myal. Hausmanni, T. helicinus, Ris. Leight, and Tur. Alten-
burgensis ; and among the other species there are also Sten. Mackrothi,
Th. dubius, and Mil. pusilla. The two assemblages have very much
in common, the principal differences being deficiencies. In both
instances Conchifers and Gasteropods are the characteristic Mollusks ;
and in both, these classes are pretty equally balanced. The all but
absence of Brachiopoda in the one, and their absence in the other, is
another point of agreement; and the representation of Polyzoa, Fo-
raminifera, and Entomostraca by species either identical or closely
related completes the similitude.

And it is quite possible, in my opinion, that this Irish group of
species may likewise have been of contemporancous existence with
the fauna with which I am comparing it. The horizon of the Cultra
and Tullyconnell beds is certainly considered to be high in the series
by Prof. King, though, with deference to the Professor’s opinion, I
would again suggest the possibility of a more appropriate classifica-

* T here argue on the usual assumption of calcareous beds being the deposition
of deeper sea than those of an argillaceous and arenaceous nature. That there
are exceptions to this it would be useless to dispute ; but as a general rule it pro-
bably holds good.

+ Journ. Geol. Soc. of Dublin, vol. vil. p. 73-78.

1861.] KIRKBY—PERMIAN, SOUTH YORKSHIRE, 323

tion. In referring these beds to the highest member of the Permian
series as developed in the North of England, Prof. King relies on
their lithological, chemical, and paleontological characters, all of
which are stated to offer a remarkably close agreement with the
equivalent features of the highest Permian member of the North of
England*. Now, in the first place, the lithological evidence of the
Upper Limestone of the North of England is of very little value as an
aid to classification. In proof of this I would refer to the Brother-
ton Beds of Yorkshire, which are as different lithologically from the
Upper Limestone of Durham as they are from any other Permian
limestone whatever, though their relative position and fossil remains
indisputably prove them to be of the same general horizon. The
lithological characters of the Upper Limestone of Durham are peculiar
to that county; and so are those of the Brotherton Beds to the ad-
joining counties of Yorkshire and Nottingham. Indeed to take the
Magnesian-limestone group as a whole, I question whether there_is
any series of rocks whose lithological characters are so variable and
of so little value in the classification of its different parts. And
so it is with the chemical composition of the Upper Limestone. Even
in Durham alone, analyses of its different beds show as great a varia-
tion in the proportion of chief ingredients as do analyses of limestones
of different members. Besides, analyses of the underlying members
sometimes so nearly agree with those of the upper, as to destroy the
worth of all arguments for the identity of age of different beds from
their similarity of chemical composition?. And in respect to the fos-
sils, there certainly does not seem to be much reason for considering
them as a group characteristic of the upper beds. Out of the 11
species that occur, 6 (viz. Sten. Mackrothi, Th. dubius, Gerv. antiqua,
Tur. Altenburgensis, Ris. Leight, and Mil. pusilla) have never been
found higher than the middle subdivision or Shell-limestone of Dur-
ham. And, as Prof. King has justly pointed out, the absence of
Polyzoa among the species occurring in the upper member i is one of
the peculiar characteristics of its faunat. For this reason I must
conclude that the occurrence of two species of this class in the Tully-
connell deposit is opposed to its being considered the equivalent of
that member. Four of the species—viz. Axv.dubius, Myal. Hausmanni,
* Loe. cit. p. 79.

+ I would Estes to the following analyses in corroboration of this assertion.
_The first is one of the Upper Limestone with which Prof. King has identified

the Irish deposit; the other is one of the Compact Limestone, the most inferior
limestone member.

Upper Limestone, Hartlepool. Compact Limestone, Ferry Hill.
Carbonate of Lime ............ 54:5 Carbonate of Lime _............ 541
OLMapnesiay ee seeeseee esas 44-9 of Magnesia ............... 44-7
Oxiderotelmonuaeree eee cece 0:3 Oxidexotslronnieteereeee en eae ee 0-6
IDEN TEOENHIETD " Gonnscounoneqatone 0-3 Harthy; matter) <......0.-..r4-<02 0-6
100-0 100-0

Greenwell’s Mine-engineering, p. 17.
+ Mon. Perm. Foss. of England, Introduction, pp. xiv, xvi; and paper ‘On
the Occurrence of Permian Magnesian Limestone at Tullyconnell, near Artrea, in
the County of Tyrone,” Journ, Geol. Soc. of Dublin, vol. vii. p. 60.

324 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 6,

Myoch. costata,and T. helicinus—are undoubtedly common to the Upper
Limestone and the Tullyconnell deposit, though likewise common to
the inferior beds ; and, had they occurred alone or with other species
also characteristic of the higher portion of the series, their evidence
would then have been more in favour of Prof. King’s suggested
classification. But, as they are associated with other species, such
as Sten. Mackrothi, Ris. Leight, and Mil. pusilla, which, in all dis-
tricts where the succession of beds has been determined, are confined
to the lower and middle parts of the series,—and as they are them-
selves among the most common species of the lower beds in some
localities, it would appear pretty certain that the balance of paleon-
tological evidence supports a classification of the Cultra and Tully-
connell beds with the inferior rather than with the superior mem-
bers of the Permian series.

§ IX. The Zechstein.—Timewill not allow my attempting compari-
sons with the groups of species found in the Zechstein of Germany; and
to do so would require a wider scope than the limit of this paper
permits. Comparisons, however, of this and of the other groups of
species found in the Permian strata of Britain with those of the
Zechstein would most assuredly bring to light many interesting facts
connected with the distribution of marine life, in time and space,
during the Permian era. The intimate relation which exists between
the marine fossils of the Permian rocks of Britain and Germany
proves them to be the remains of one fauna peopling the same geo-
graphical province or area of deposition. And to trace the various
phases in the history of this fauna, its peculiarities of distribution
in space and in time, its development, and manifold relations, will
certainly be the work of some paleontologist when our knowledge
of it and the strata containing it becomes more advanced.

§ X. Conclusion. Distributionof the Permian Fauna in Time.—After
the deposition of the Lower Limestone and during that of the Small-
grained Dolomite, it would appear as if there had been a total with-
drawal of species from the South Yorkshire area. During the same
period in Durham the Permian fauna was at its maximum. Thus
we have another most remarkable instance of local difference in the
geographical distribution of Permian species.

This exodus of species was in most cases permanent. Only two
are known to return during the deposition of the Brotherton Beds.
Others may certainly be undiscovered ; but so far as we know Awinus
dubius and Myalina Hausmanni, accompanied by one, or perhaps
two, species of Alge previously unknown, are the only ones that
revisit the South Yorkshire area. During the early part of the same
period a few other species were associated with these in the nearly
adjoining region of Durham. But the Durham fauna, like that of
Yorkshire, was greatly reduced in number, both specifically and
individually, compared with its development in the preceding epoch.
Out of its 118 Shell-limestone species only 22 reappear in the Upper
Limestone, 6 new species appearing along with them. In the highest
portion of this member (at Roker and Hartlepool), the only species
that occur are the two Conchifers found in the Brotherton Beds, and

mit!
Na A
Wey

oD
bis

J.WX del, Geo. West. ith.

PERMIAN FOSSILS FROM YORKSHIRE.

1861. | BUNBURY—FOSSIL PLANTS, NAGPUR. 320

Turbo helictnus. In the equivalent strata of the Zechstein there is
a similar falling off in the distribution of species ; and the same forms
are the characteristic fossils there, Aw. dubius under its “ Schlotheimi”
character being the most common. It would thus appear that in
the whole of the West European area there was a most remarkable
decrease in the Permian fauna during the period of deposition of the
Upper Permian strata, the decrease being greater towards the close
than at the beginning of that period, and affecting the same classes,
and even the same species in most cases, in the different parts of
that area, thus leaving a similar though exceedingly meagre group
of species distributed throughout.

EXPLANATION OF PLATE VII.

Figs. 1, 2, 4, 5,6. Rissoa Leight, Brown. Five specimens illustrative of its
variation of form; magnified about 14 times. Hampole.

Fig. 3. Rissoa Leight, Brown. Young individual ; magnified 16 times. Hampole.

Figs. 7,8. Natica minima? Brown. Outer lip of specimen imperfect; mag-
nified 12 times. Hampole.

Figs. 9, 10. Turritella Altenburgensis, Geinitz. Magnified 16 times. Hampole.

Fig. 11. Axinus dubius, Schlotheim. New variety. Cast; somewhat enlarged.

Moorhouse.
Fig. 12. Axinus dubius, Schlotheim. New variety. Cast; somewhat enlarged.

Conisborough.

Marca 20, 1861.
The following communications were read :—

1. Notes on a Cotrection of Foss Prants from Niepur, CENTRAL
Inpra. By Sir Cuartezs J. F. Bunsury, Bart., F.R.S., F.G.8., &e.
[Plates VIII—XI1.]

Introduction.—It is now some considerable time since the fine
collection of fossil vegetable remains from the district of Nagpur in
Central India, which had been presented to the Geological Society
by the Rev. Messrs. Stephen Hislop and Robert Hunter*, was en-
trusted to me for examination and description. Owing to the obscure
and equivocal character of many of these remains, the undertaking
proved more tedious than I had expected, and there still remain
many specimens to which I have not yet been able to give a thorough
examination. But, as particular circumstances make it unlikely
that I should, for some time to come, have sufficient leisure to
devote to this pursuit, I think it best to lay before the Society at
once the results of my inquiries as far as they have yet gone, rather
than to keep them back for an indefinite time in the hope of com-
pleting them. The present paper, therefore, will contain the descrip-
tion of all the Ferns in the collection, and of all those remains of
Stems and Leaves of other kinds which I have, to the best of my
ability, sufficiently examined; these altogether constitute nearly

* See Quart. Journ. Geol. Soc., vol. xi. p. 348 and p. 369.

326 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

three-fourths of the collection. The Fruits and Seeds, of which the
specimens are pretty numerous, but obscure and difficult to determine,
are reserved for further examination. I may observe, however, that,
though numerous in individuals, they seem to be little varied in form
and character, and present no outward evidences of a high organiza-
tion.

The general remarks which form the latter part of this paper
are founded, I must observe, not merely on the close examination
which I have given to the specimens herein described, but on a
general survey of the whole. It is possible that a more minute
examination of the remaining fossils (the Fruits and Seeds) may
partially modify some of the conclusions I have drawn,—but not, I
think, to any very material extent.

FERNS.

1 (a4). Grossopreris Brownzna, var. Indica, Ad. Brongn. Hist. Vég.
Foss. p. 223, pl. 62. f. 2. Pl. VIII. figs. 1-4.

This, as appears from the very numerous specimens in the collec-
tion, is one of the most common plants of the supposed Jurassic beds
of Nagpur. Excepting one doubtful fragment from Kdmpti, all the
specimens are from Silewdda, and are very numerous, of large size,
and in a fine state of preservation ; yet even among these it is not usual
to find a frond with both extremities perfect. One specimen, though
broken at both ends, still measures 14 inches in length, and must
have measured at least 17 inches when perfect. Another (almost
perfect) is 14 inches long; the largest I have seen is 16 inches
long in its present state (with the apex broken off), and must cer-
tainly have been 18 inches. On the whole, from a comparison of
numerous specimens from this locality, we may say that the full-
grown fronds were from 10 to 18 inches in length (exclusive of the
stalk), and seldom more than 23 inches in their greatest breadth.
The outline of the frond in all these fine specimens from Silewdda
is narrower, more lanceolate, and more tapering to a point, than in
Brongniart’s original Australian plants, and even than in his figure
of the Indian variety (pl. 62. fig. 2). Like the Australian plant,
however, it always tapers very gradually to the base, passing almost
insensibly into the stalk (of which but a small portion is preserved in
any specimen that I have seen) ; and the greatest breadth is generally
above the middle. The apex of the frond, wherever it is preserved,
always tapers regularly into a very acute point.

The midrib is remarkably broad, but flattish, and not very promi-
nent, strongly striated, tapering very gradually upwards, and reaching
quite to the point. Morris long since remarked (in Count Strzelecki’s
‘New South Wales,’ p. 248) that the venation of the specimens
examined by him did not altogether agree with Brongniart’s deserip-
tion, and that the reticulation of the lateral veins was not confined to
the neighbourhood of the midrib, but that they anastomosed
repeatedly at various distances between the midrib and the margin.
Brongniart has since repeated (in his ‘Tableau des Genres de Vég.
Foss.’) his original character of the genus, without taking any

1861. | BUNBURY—FOSSIL PLANTS, NAGPUR. 327

notice of Morris’s remarks. My observations, however, both on the
Nagpur specimens and on the numerous Australian ones which I
have examined, agree with those of Morris. The lateral veins
(which are very fine and close) are repeatedly forked near the
midrib, and there form, by the anastomosing of their branches, a
conspicuous reticulation, of which the meshes are somewhat oblong.
Towards the margin they become nearly parallel, forking very
sparingly, and anastomosing at long intervals, so as to form very
long and narrow meshes; but still they do anastomose here and
there, even to the margin. The venation of the New South Wales
Glossopteris agrees in these characters with that of the Indian plant ;
and one of Brongniart’s figures (fig. 1 a, pl. 62) represents the veins
correctly, though somewhat at variance with his own description.

In the Nagpur specimens which I refer to this species, I find
some degree of variation in the fineness and closeness of the veins—
such an amount of difference, indeed, occasionally, as might at first
sight seem to imply a distinction of species ; but there are so many
intermediate gradations that I do not find it possible to draw the
line. I think it probabie that these differences may depend partly
upon the age of the frond, partly, perhaps, upon various conditions
attending the fossilizing process, as I have observed that the apparent
closeness of the veins in some recent Ferns is influenced by circum-
stances in the process of drying.

The position of the fructification is indicated in several of these
specimens by small round spots, very regularly arranged in 1 or 2
rows parallel to the margin—the outermost row at but a short
distance from the margin, the inner about half-way between the
outer and the midrib. When there is only one row, it is always
the inner one that is wanting. In these spots I can find no organic
structure at all, but only little lumps of the sandstone, as if not only
the sori themselves, but the very substance of the frond had decayed
or been displaced at these points. I think, however, from the regu-
larity of their form and arrangement, there can be no doubt that
they really indicate the places af the sori.

I perceive no trace of scales on the midrib or stalk of even the
best-preserved specimens.

M. de Zigno has expressed an opinion that the Glossopteris Brown-
wana had a compound or digitate frond, as the allied Sagenopteris
Phillipsti had; indeed, he quotes a report that a specimen had been
found to establish this fact. I confess, however, that I can find
nothing in corroboration of his opinion. Among the numerous
specimens I have examined of the Indian Glossopteris (some of the
large slabs of stone from Silewddd containing as many as ten or
twelve fronds), I can see nothing to indicate that the leaves were
portions of a divided or lobed frond, or were otherwise than simple
fronds, like those of our Hart’s-tongue Fern, or of the Bird’s-nest
Asplenium (A. mdus, L.). Neither can I find any different struc-
ture in this respect in the Australian specimens of Glossopteris that
I have seen, nor does McCoy mention any in his memoir.

Dr. McClelland (Report of the Geological Survey of India, 1850) has

328 PROCEEDINGS OF THE GEOLOGICAL society. — { Mar. 20,

indeed figured* a specimen of G'lossopteris which might at first sight
be supposed to show a digitate form of frond; but on examination
of the drawing, it is clear that the leaves did not all grow in the
same plane, and that, instead of being leaflets of a digitate frond,
they are really simple fronds growing in a tuft (as is so common in
recent Ferns) from a short thick rhizoma. His description, too,
though not very clear, sufficiently indicates that he understood the
structure as I do. Such a specimen, nevertheless, ill understood,
may easily have given rise to the report quoted by De Zigno.

Notwithstanding this difference in the composition of the frond
between the typical species of G'lossopteris and of Sagenopteris, I yet
agree with De Zigno in doubting whether the two genera are suffi-
ciently distinct. In specimens of Sagenopteris Phillips from
Scarborough, I find the venation so similar to that of the Australian
Glossopteris, that it would be very difficult to found a generic differ-
ence upon this character. Some of the Indian forms of Glossopteris
certainly depart more widely from Sagenopteris in their venation ;
but there are others again, as I shall presently mention, which show
truly intermediate characters. The fructification of Sagenopteris is
still entirely unknown ; and it is possible that, when discovered, it
may prove the two genera to be quite distinct; but in the present
state of our knowledge, I see no sufficient reason for keeping them
separate.

If it be thought expedient to reunite these genera, the name of
Glossopteris certainly ought to be retained, as the older and per-
fectly unobjectionable.

On comparing this Indian Glossopteris with the common Austra-
lian G. Browniana, allowing for the apparent differences produced
by the nature of the stone and the state of preservation of the
specimens, I can find no satisfactory specific distinction; the
venation is essentially the same. We may indeed find Indian speci-
mens in which the meshes of the reticulation near the midrib are
larger and broader than in the ordinary Australian plant, and others
in which the veins are more strongly recurved; but, in both the
Indian and Australian plants, I find so many shades of variation in
these particulars, that I cannot attach much importance to them.
The general form varies considerably in the Australian specimens,
and is often quite as narrow as in those from Nagpur; the apex
also varies in the Australian plant, from very obtuse, and even retuse,
to rather acute, though I admit that it is never, in the specimens I
have seen, as acute as in the Indian. I have seen no trace of fructi-
fication in Australian specimens, nor is any mentioned by McCoy ;
on the other hand, I am unacquainted with the rhizoma of the
Indian Gilossopteris. In the absence of these important points of
comparison, we cannot feel certain of the specific agreement of the
two.

With respect to the affinities of Glossopteris to recent Ferns, I
am not able to add anything to what Brongniart has said. The
form and position of the sori indicate its place either in the tribe of

* PL. 14. fig. 3.

1861. | BUNBURY—FOSSIL PLANTS, NAGPUR. 329

Polypodiew or of Aspidiew ; but no recent genus of either of those
groups has the same venation. In this latter respect some of the
Acrostichew approach nearer to Gilossopteris ; but the reticulation of
their veins is always more uniform.

Among fragments of fossil plants from Bloemkop, South Africa,
collected by Dr. Rubidge, and exhibited before the Geological Society
Noy. 17, 1858, there are two forms which appear allied to Glosso-
pteris,—one a narrow, somewhat lanceolate frond, with veins nume-
rous and very fine, resembling in direction those of G. Browniana,
not very evidently anastomosing (but this was perhaps rendered ob-
secure by the bad state of the specimen); the other consisting of
mere fragments, with veins forming a lax and regular network—
perhaps more like the venation of Dictyopteris than of Glossopteris.

1 (@). Guossopreris Brownzana, var. Australasica, Ad. Br. Hist.
Vég. Foss. pl. 62. fig. 1. Pl. VIII. fig. 5.

I find two specimens which have the form usual in the Australian
specimens and considered by Brongniart as typical of the species—
namely, tongue-shaped or subspathulate, with an obtuse apex. Both
are small: the larger, in fine reddish-white sandstone from Bharat-
wada, is 53 in. long, 1? in. in maximum breadth; the other (in a
coarse, blackish, micaceous sandstone from the foot of the Mahddewa
Hills) 33in. by lin. Venation rather ill preserved and indistinct in
both, but apparently agreeing with the Australian specimens.

2. GLOSSOPTERIS MUSHFOLIA, n. sp.? Pl. VIII. fig. 6.

Several specimens of a Glossopteris, both from Silewdda and from
Kampti, appear to belong to a different species from that first
described, though none of them are complete enough to be quite
satisfactory. The direction of the veins, which (unless very near
their base) are straight, and almost perpendicular both to the midrib
and to the margin, might cause the plant to be taken for a T'enio-
pteris; but these veins are in fact dichotomous, and anastomose
repeatedly near the midrib. They are extremely numerous, very
fine and close, and for the greater part of their length quite parallel.
Besides, the frond is much broader than in G. Browniana (3 to 4
in. broad), and appears to have been quite rounded at the apex; the
actual apex however is not perfect in any specimen that I have seen,
nor do any show the form of the base. The frond appears to have
been of thin substance, and apt to split or tear transversely in the
direction of the veins, like the leaves of the Banana (Musa). One
specimen shows remains of fructification in round spots, arranged
as in G. Browniana.

Ferns are so variable that I feel some doubt whether this may
not hereafter prove, when better known, to be a variety of G.
Brownana. I think I see in some specimens a tendency to inter-
mediate gradations of character; yet in living Ferns, as far as I
have been able to observe, the direction of the veins appears to be
very constant in each species, even in such variable plants as Scolo-
pendrium officmarum and Asplenium nidus. As the characters of

330 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

the present plant are sufficiently striking, I think it best to distin-
guish it, provisionally, as a species. It may be characterized as
follows :—

Glossopteris muscefolia.

Frond broadly oblong, rounded and very obtuse at the apex ; side-
veins very slender, very much crowded, dichotomous, nearly perpen-
dicular to the midrib and the margin, near the base only oblique
and anastomosing.

Glossopteris frondosa, McClelland*, has some resemblance to this,
especially in general form; but neither the figure nor the descrip-
tion enables me to identify the two. If they be the same, the most
important characters of the venation are overlooked by that author.

3. GLOSSOPTERIS LEPTONEURA, n.sp.? Pl. IX. figs. 1-4.

Numerous specimens in sandstone from Kdampti; the fronds
generally in great numbers on the surface of each slab of sandstone,
lying confusedly together, so that hardly any frond is visible in
its whole length: it appears that the plant must have grown in
great abundance in particular spots. I at first took this species for
the Glossopteris angustifolia, Ad. Br., which it resembles in outline ;
but, judging from the figure and description of that speciest, the
venation is essentially different. In G. angustifolia, the veins ap-
pear to be coarse and rather distant, and sparingly anastomosing
near the midrib only; in our Kampti plant they are very fine and
close, and anastomose repeatedly throughout their length, even near
to the margin, forming almost as regular a network as in Sageno-
pteris Phillips. Our plant agrees more nearly (indeed very nearly)
with G. linearis, McCoy; but the veins are much more oblique
than they are described in that species, and quite as much so as in
G. angustifolia.

The frond of this Glossopteris is, like that of G. linearis, very
narrow in proportion to its length, with nearly parallel margins;
some of the most nearly complete specimens are 43 to 6 inches
long, with a breadth of only half an inch; the apex acute, but less
remarkably so than in the Nagpur form of G. Browniana ; the base
tapering very gradually into the footstalk.

One very small frond, from Kampti, apparently a young plant of
this species, has preserved the whole of its leafstalk or stipes, which
I have not seen in other instances; this stipes is much shorter than
the frond, narrow, and rather suddenly dilated at the base.

Intermixed with the narrow linear fronds which I have deseribed,
I find others, in much smaller numbers, of a broader form, lingulate
or somewhat lanceolate, but with precisely the same venation as the
narrow ones. They have the form of G. Browniana Indica, but are
still, I think, clearly distinguishable by their finer veins and the
more uniform reticulation of these veins,—the venation, in fact, being
that of Sagenopteris. These broader fronds appear to me to belong
to the same species with the narrow linear ones: it may be doubted

* Report of Geol. Survey of India, p. 55, pl. 15. f. 3.
+ Ad. Brongn. Hist. Vég. Foss. 224, pl. 63. f. 1.

1861.] BUNBURY—FOSSIL PLANTS, NAGPUR. Bel

(as in the case of the narrower and broader fronds of Sagenopteris
Phillipsit) whether the two are to be considered as varieties, or
(which I am rather inclined to believe) as two different forms of
frond which may occur on the same plant, as many recent ferns
have biformed fronds. I can find no trace of fructification on any of
the specimens of G. leptoneura; nor, again, is there anything to
indicate that they were otherwise than really simple fronds.

If Sagenopteris is to be distinguished as a genus from Gilossopteris
by its venation, the present species will be referable rather to the
first of these genera; but it appears to me that this and the G.
linearis, McCoy, are rather to be considered as connecting links tend-
ing to reunite the two supposed genera.

The distinctive characters of my Gilossopteris leptonewra may be
thus expressed :—

Frond narrow, nearly linear (qu. sometimes lanceolate ?), rather
acute at the apex, tapering very gradually at the base into the stalk.
Midrib narrow, continued to the apex. Side-veins very fine, very
oblique, arched, dichotomous, anastomosing, and forming a complete
network from the midrib to the margin.

4, GLOSSOPTERIS STRICTA, n. sp.? Pl. IX. fig. 5.

Of this there are very few specimens; but the plant appears a di-
stinct one, almost ambiguous in characters between Gilossopteris and
Teniopteris—at first sight more resembling the latter. Midrib very
broad and strong. Lateral veins very numerous and close, perpendi-
cular to the margin (as in T'eniopteris) and almost straight, only a
little arched at the very base; more than once forked, and anasto-
mosing near their base—that is, near the midrib. This venation agrees
pretty closely with that of G. musefolia, No.2; but the frond is of
a different form, narrow, strap-shaped, with nearly parallel edges,
only very slightly widening upwards; it has a much more firm and
rigid appearance, showing no tendency to be waved or crumpled.
The best specimen (with both ends broken off) is 9 inches long, and
rather more than 1 inch in greatest breadth. The anastomosing of
the veins is most apparent in the lower part of the frond.

Loc. Silewada and Kampti.

5. Precorpreris? Pl. IX. figs. 6-8.

A single specimen from Kdmpti. A doubtful Pecopteris, with con-
siderable resemblance in outline, and apparently also in the venation
(which however is very obscure), to P. Plukenetii, Ad. Br. The speci-
men is ill preserved ; but the frond appears to have been large and
very compound—tripinnatifid at least. The portions which are pre-
served are probably the upper or terminal part of the frond (which is
bipinnatifid) and two of the lateral pinne or branches (also bipinna-
tifid). Main rachis slightly winged or bordered. Pinne (of the
second order) long, nearly linear in their general outline, spreading
nearly at right angles to the main rachis, pinnatifid; ultimate pin-
nules nearly round (rounder than in any form of P. Plukeneti figured
by Ad. Br.), alternate or, in parts, nearly opposite, united from their
base nearly half-way up, entire, diminishing very gradually towards

332 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 20,

the extremity of the pinna; the terminal one small, roundish, not
much separated from the next. Veins (very indistinct in the speci-
men) scarcely agreeing with the generic character of Pecopteris, but
well enough with those of P. Plukenetu, as represented by Ad.
Brongniart, tab. 107. fig. 3.4; midrib faint, not reaching to the
apex, but breaking into very oblique and repeatedly forked side-
veins.

In outline this plant strongly resembles Odontopteris Schlotheimi,
Ad. Br. t. 78. f. 5, except that the pinnules are smaller and more
numerous on each branch; but the veins are quite different. The
venation approaches to that of some species of Sphenopteris ; but the
plant cannot well be referred to that genus, for the form and position
of the pinne and pinnules are those of a Pecopteris of the section
Unite. Ithas much resemblance to a fern from the anthracite-slates
of Savoy (No. 9 of my paper in Quart. Journ. Geol. Soe., vol. v.
p. 140), which is referred by Heer to Pecopteris Plukenetti. One of
McClelland’s* figures of his Pecopteris affinis (pl. 13. fig. 11 6) has
a resemblance in outline to this plant ; but the figure is too imperfect
to allow of identification.

6. Crapopuiesis, Pl. X. fig. 1.

A very small fragment of a Fern (from Kaémpti), not to be named
or identified from such very imperfect materials, perhaps belonging
to Pecopteris Lindleyana (of which I have seen no specimens nor
satisfactory description), evidently different from any other in this
collection. It may be referred to Brongniart’s genus Cladophlebist
(corresponding to Pecopteris, section Newropteroides, of the Hist. Vég.
Foss.), the venation being intermediate between that of Neuropteris
and of Pecopteris. Pinnules about as large as those of Newropteris
Loshii, and a good deal like them in shape, but more oblique; the
base not cordate, but oblique or unequal-sided, and (as in Clado-
phlebis pteroides) only partially attached to the rachis. Midrib
more continuous than in Neuropteris, but less than in the typical
Pecopterids ; side-veins very oblique, but less arched, less crowded,
and more sparingly branched than in Neuropteris proper.

I find another fragment from Kémpti, which I am inclined to refer
to this same plant, although it is in a state which renders its deter-
mination doubtful. It appears to be a portion of a Fern, with the
leaflets reduced (probably by decay previous to fossilization) to a
skeleton, little else remaining of them than the veins; whence the
fragment might be taken at first sight for some delicate Sphenopteris.
It is well known that the Sphenopteris myriophyllum, Brongn., was
founded on a specimen in a similar condition.

7. TNIOPTERIS DANHOIDES, McClell.? (Glossopteris dancoides,

Royle?) Pl. X. fig. 2.

The specimens of this (in sandstone from Kémpti) are but few and
very imperfect; but they belong (as far as can be seen) to Brong-
niart’s genus Teniopteris, and may be the same species with the

* Report of Geological Survey of India, 1850.
+ Tableau des Genres des Végétaux Fossiles.

1861.] BUNBURY—FOSSIL PLANTS, NAGPUR, 333

Glossopteris danceoides of Royle, which is very properly referred by
McClelland to Teniopteris. This Nagpur plant has also a striking
resemblance (as far as can be judged from such fragments) to the
Teniopteris major, L. and H.; but the imperfect state of our mate-
rials does not allow us to identify them.

Is it not possible that this plant, and also the Teniopteris major,
may belong to Oycadce, or at least to the same family with Ptero-
phyllum? Dr. Murray, of Scarborough, first suggested this to me
while comparing the specimens of Pterophyllum comptum, L. & H..,
with those of Teniopteris in his collection. In one of his specimens,
the lower half of the leaf has the characteristic form and division of
Pterophyllum comptum, while the terminal half is altogether undi-
vided and has the appearance of a Tewniopteris. Another specimen
might be taken for a Teniopteris, but shows towards its middle a
tendency to split into pinnules.

8. Finicitzs. Pl. X. fig. 3.

A small frond, from Silewdda, unfortunately too imperfect to be
satisfactorily described or referred to its proper genus, but curious.
At first sight it might be taken for a small specimen of Batera Hut-
toni, Ad. Br. (Cyclopteris digitata, L. & H.); but the venation is
quite different: instead of numerous, equal, regularly radiating,
dichotomous veins, it has a single well-marked midrib in each lobe ;
the lateral veins extremely indistinct, but apparently going off very
obliquely from these ribs. The lobes preserved in this specimen are
four in number; but there were probably seven, gradually diminishing
in size each way from the middle one ; not very deeply separated, of
an obovate oblong form, and very obtuse. Base of frond wanting.
Mr. Hislop has labelled this specimen as “ small Glossopteris ;” and
I think it not impossible that it may belong to a seedling plant of
Glossopteris ; but there is no evidence to connect it satisfactorily with
that genus.

9. Fruicrres (qu. Guossopreris, sp.?). Pl. X. fig. 4.

This is unfortunately a very imperfect fragment, but of a curious
plant, unlike any other I have seen in a fossil state,—undoubtedly a
Fern, but scarcely referable to any genus hitherto established ; there-
fore, rather than attempt to found a new genus on such imperfect
materials, I leave it under the vague name of Filicites. It is from
Kampti.

Stipes (incomplete) 2? inches long in this fragment, very broad
and flat, bearing in its upper part three leaves or leaflets on one side
and one on the other (the others which ought to have been on this
side being destroyed). Leaflets very incomplete, more than half of
each being broken off; but they appear to have been of considerable
size, entire and undivided, and probably of an oblong or lanceolate
form—not, however, tapering gradually into a stalk as in Glosso-
pteris, but sessile on the main stalk, attached to it by a broad oblique
base ; closely placed, so as partly to overlap one another, and appa-
rently increasing progressively in size upwards, the lowest being
smallest. The venation is very ill preserved and very indistinct, but

334 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

appears nearly, if not quite, that of Glossopterts. Midrib narrow but
sharply marked; side-veins numerous, fine, oblique, but scarcely
arched, sparingly dichotomous ; and I think they occasionally anasto-
mose ; but thisis not very distinct. Texture of the frond seemingly
thin.

This may possibly be a genuine Glossopteris, but differs remarkably
from those hitherto described in the composition of its frond. It
certainly cannot be a state either of G. Browniana, or of any of the
other species described in this memoir. Even supposing the appa-
rently simple fronds of these species to be leaflets of a compound
frond (which is very improbable), they are constantly characterized
by a form much narrowed towards the base, and tapering very gradu-
ally into a petiole of some length; whereas in this, the leaflets
neither taper gradually to the base, nor have any partial stalk, but
are attached at once by a broadish base to the main stalk.

10. Naecrratuia ? (Cyciopreris?) Histopi,n.sp. Pl. X. fig. 5.

The leaves, or (as is perhaps more probable) detached leaflets,
which occur in several pieces of stone from Bharatwdda, and which
Mr. Hislop has marked as “ Cyclopteris,” appear to me to belong
rather to the genus Neggerathia, or at least to the family of Neg-
gerathiee of M. Brongniart. None of the specimens are nearly com-
plete; but by a comparison of different fragments we see that the
leaf was of a narrow wedge-shape, widening gradually upwards from
a narrow base—not however quite symmetrical, but very slightly
oblique; the terminal portion, which is well seen in one fragment,
very conspicuously oblique, rounded at the actual apex, and from
thence sloping away with a gentle curve, and forming a very obtuse
and rounded angle with the other (lower) margin. The leaf (as far
as can be judged from mere impressions) appears to have been of a
firm and rather rigid texture, with a smooth surface. The largest
fragment I have seen is about 523 inches long; the breadth in no
part seemingly much exceeding 1 inch. Veins numerous, all equal
and uniform, with no appearance of a midrib, strong and rather
coarse, radiating from the base, but spreading very gradually and
forming very small angles with one another, so that for any short
distance they appear nearly parallel; they are once or twice forked,
but very sparingly, the branches diverging very gradually, and all
end in the terminal margin.

This plant may very possibly be a Fern; but the same reasons
which led M. Brongniart to consider the Neggerathia as allied to
the Cycads induce me to think that this also is rather to be
ranked with that family than with the Ferns. The forked veins,
indeed, are unusual in Cycadew, but in Ceratozamia Mewicana the
veins are occasionally forked, and in Stangeria paradoxa they are
constantly so. In the genus Otopteris or Otozamutes, which M,
Brongniart refers without doubt to Cycadec, the veins are regularly
and repeatedly forked; at least, such is the case in Otozam. acumi-
natus and O. obtusus. The breadth and coarseness of the veins in our
Nagpur plant, and a certain appearance of rigidity about the leaf,

1861.] BUNBURY—FOSSIL PLANTS, NAGPUR. 330

look to me rather like a Cycad than a Fern. All these reasons, how-
ever, are far from conclusive ; and I must admit that, to me, it still
remains a matter of much doubt to which of the two families this
plant should be referred. If a Fern, it must from its technical charac-
ters be placed in Cyclopteris, although it evidently has no natural
affinity to any of the plants comprehended under that name. It
might be named Cyclopteris Hislopia.

The dichotomy of the veins, their equality and uniformity, and the
absence of any trace of transverse connecting veins, plainly show
that it is not a Palm.

A small leaf or leaflet in sandstone from Kimpti agrees with this
in venation, and evidently belongs to an allied species, perhaps not
to the same ; for the outline is different, being in the Kampti plant
lanceolate and nearly symmetrical, instead of cuneiform and oblique.
This specimen is better preserved than those from Bharatwad#, and
shows the form of its base, though not its actual connexion with the
stalk or stem; there is an appearance of thickening at the base, as
is seen in several of the Cycadew, and some indication of its having
been connected with the stalk by an articulation. The leaf appears
to have been of a thick and leathery texture; the veins are rather
indistinct; the surface appears minutely granulated, but I am not
quite certain whether this is really owing to the texture of the leaf
itself. This specimen may probably belong to a distinct species ;
but our materials being so very imperfect, I do not think fit to give
it a separate name.

A specimen, apparently belonging to this plant, from Tondakheiri,
has been labelled “ Cyclopteris with fructification.” It is not in a
good state of preservation; the apex appears wrinkled or thickened ;
the veins (or the spaces between the veins) swollen and distorted,
and as it were knotty or granulated at their extremities. This ap-
pearance has been taken for fructification ; and if it were so, there
could be no doubt of the plant being a Fern. But I confess that, on
a close and careful examination, I can see nothing sufficiently distinct
and definite to satisfy me that this peculiar appearance can be re-
ferred to fructification. The specimen unfortunately is ill-pre-
served; it exhibits merely an impression—and not a sharp or clear
one—of the original in a sandstone not of very fine grain; and [
think it possible that the swollen and wrinkled appearance at the
apex of the leaf may be produced accidentally by something in the
nature of the stone or the process of fossilization. The evidence of
its being the fructification of a Fern is not at present sufficiently clear
to me to overcome the reasons which induce me rather to refer the
plant to Cycadee, or a neighbouring family.

Plants of doubtful Affinity.

11. Payriorgeca Inpica, C. B. Pl. X. figs. 6-9; and Pl. XI.
figs. 1 & 2.
Specimens are numerous in the fine-grained sandstone from
Bharatwada ; all very fragmentary, but some of the fragments deli-
VOL. XVII.—PART I. 24

336 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

cately preserved. There are other specimens also from Bokhdara,
Kadmpti, Silewada, and Barkoi. It is difficult to form a clear idea
of the general form and habit of the plant; but the specimens
give satisfactory information as to the leaves and sheaths, their rela-
tive position and connexion. Some of them show conclusively the
accuracy of Brongniart’s original statement, that the leaves are pro-
longations of the teeth of the sheaths. Lindley (followed by Unger
in his ‘ Synopsis’) conjectured that Brongniart had been deceived, and
that the leaves really surrounded the sheath, springing from below
it ; but the correctness of the original description has been confirmed
by the observations of Morris* and McCoy,t on specimens from
New South Wales; as well as by the later ones of Baron Achille de
Zigno on two new species of the genus discovered by him in the
Jurassic rocks of the Veronese territory t. The specimens before me
are, I believe, the first that have been described from India§. They
were very correctly referred by Messrs. Hislop and Hunter to the
genus Phyllotheca ; and it is not yet clear to me whether they are
even specifically distinguishable from those of New South Wales.
Some of these fragments show most unequivocally the continuity
of the narrow leaves with the sheaths; that, in fact, the leaves are
simply the elongated teeth of the sheaths ; or, to express it in a dif-
ferent way, that the sheaths are formed of the united bases of the
leaves. The sheaths in this Bharatwida plant are not closely
pressed to the stem, as described in the original Phyllotheca australis
of Brongniart, and in McCoy’s P. ramosa; they widen more or less
rapidly upwards, and more rapidly in the upper part, so as to be
somewhat funnel-shaped or bell-shaped; on the upper parts of the
small branches they appear to cover the whole, or nearly the whole,
length of the internodes. These sheaths are strongly and regularly
furrowed; the furrows appear to correspond in number to the leaves,
and to be prolonged into their midribs. Leaves numerous in each
whorl, but I have not yet found any specimen sufficiently perfect to
show their exact number ; they are linear, very narrow, longer than
the sheaths, with a distinct midrib; in direction sometimes erect,
more often spreading at various angles, and very often recurved.
The sheaths seem to be deciduous; at least I can find no trace of
them on what appear to be stems and older branches of the same
plant, which are regularly and distinctly furrowed and jointed, like
a Calamites. The furrows do not, however, alternate at the joints,
as in all the Calamites except C. transitionis Gopp.; the ridges and
furrows of each internode are in the same line with those of the next.
McCoy describes the branches of his P. ramosa as originating
“« directly over the joints,” and being therefore “ within and axillary
to the sheaths.” The same is evidently the case with P. Brongni-
artiana of De Zigno. Some of the Nagpur specimens show branches,

* Strzelecki’s New South Wales, p. 251.

+ Annals of Nat. History, v. p. 20 (1847).

{ Flora Fossilis Formationis Oolithice, pp. 59, 60, tabb. 7, 8.

§ No species of Phyllotheca is noticed by McClelland in his enumeration of
Ae, an fossil plants (Report of Geol. Survey of India, Calcutta, 1850).

1861.] BUNBURY—FOSSIL PLANTS, NAGPUR. 337

but unfortunately their origin relatively to the sheaths is obscure ;
for they spring from what appear to be the old stems, on which I
ean find no sheaths remaining. They are inserted on the stem with
a distinct articulation, as in Hquisetum and Calamites; but their
insertion appears to be exactly on the articulation of the stem, and
not below it. In the P. ramosa and P. Brongniartiana, the origin
of the branches is unequivocal; and, though less evident, it is pro-
bably the same in this plant. I think, with McCoy, that this cha-
racter decidedly removes Phyllotheca from any near affinity with
Equisetum, as one of the especial and most peculiar characters of
the latter genus is the origin of the branches from below the sheaths.

Some further light is thrown on this question by a specimen*, from
Silewida near Nagpur, of what appears to be an old stem of a small
Phyllotheca; the arrangement of the ridges and furrows being such
as is usual in this genus, and not such as prevails in Hquisetum and
Calamites. Here there is a scar, doubtless of a branch, seated exactly
on one of the articulations, and perfectly similar, except in its small
size, to what we see in Calamites ramosus, Ad. Br. No trace of a
sheath remains.

Some of the flattened stems, which I suppose to belong to this
Phyllotheca, are above an inch broad, strongly and coarsely furrowed.
As they are pressed quite flat, without being crushed or distorted, we
must suppose either that they were of a soft and herbaceous sub-
stance, or that the wood had entirely decayed before they were
fossilized, leaving only a tube of bark.

It is not improbable that the remains of Phyllotheca in this Nag-
pur collection may belong to more than one species, as the great
difference in the fineness or coarseness of the furrows on stems of
about the same diameter may seem to indicate; but I cannot satisfy
myself as to the distinctions.

Our materials being still so incomplete, I feel by no means sure
that further discoveries may not prove this Indian Phyllotheca to be
identical with one or other of the Australian species. Yet, as it
does not ewactly agree with the description of any of them, and as
there is a prima facie probability that plants from such distant coun-
tries are not the same, I will provisionally name this one Phyllotheca
Indica.

Its characters may be given thus :—

Stem branched, furrowed; sheaths lax, somewhat bell-shaped,
distinctly striated; leaves narrow linear, with a strong and distinct
midrib, widely spreading and often recurved, nearly twice as long as
the sheaths.

The original Phyllotheca australis, Brongniart, and the P. ramosa,
McCoy (according to the descriptions), differ from this in having the
stem smooth or slightly striated, not furrowed, and the sheaths fitting
closely to the stem; P. australis further in its simple stem, and
leaves withouta midrib. P. Hookeri, McCoy,which of the described
species comes nearest to our Indian one, appears to have much larger
sheaths and longer leaves, as well as a simple stem.

* See PI. X. fig. 6.

2 2,

338 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

The real affinities of Phyllotheca to existing plants are scarcely to
be determined in the present state of our knowledge. It appears,
as Brongniart observes, to be nearly allied to the fossils called Astero-
phyllites and Annularia, and most probably also to Calamodendron,
Ad. Br.,—all these having essentially similar characters of ramifica-
tion, with verticillated one-ribbed leaves. The position of the
branches shows that it cannot be nearly akin to Hquisetacee.
McCoy’s arguments to prove it a near ally of Casuarina, do not
appear to me conclusive. The catkin which he has figured as the
male flowers (see his pl. 11. fig. 1), strikes me as agreeing well
enough in its general structure with the known fructification of
Asterophyllites and Annularia (see Geinitz, ‘Steinkohlenform.
Sachsen,’ tab. 17. fig. 3, tab. 18. fig. 8,9). No other kind of fructifi-
cation, as it seems, has yet been found in connexion with any Phyl-
lotheca. If these plants belonged to the group of the Casuarina, it
is hardly probable, abundant as they are, that some trace would not
have been found of the remarkable seed-vessels of that family.

12. VerteBRARIA? PI, XI. fig. 3.

Some impressions in sandstone from Kzmpti, Tondakheiri, and
the Mahadewa Hills, and in bituminous shale from Barkoi, labelled
as “ Vertebraria,”’ have certainly a primd facie resemblance to the
published figures of the Vert. Indica, especially to that in McClel-
land’s Report, tab. 14. fig. 1; but I can hardly reconcile the appear-
ances presented by these specimens with the structure described by
McCoy and De Zigno. The specimens indeed appear to be merely
impressions, consequently not showing a transverse fracture, nor
exhibiting anything of the radiated structure described in Verte-
braria. But the Kampti specimens are branched, a circumstance not
hitherto recorded in any Vertebraria; and branched in a manner
which I cannot reconcile with the received explanation of the struc-
ture of that genus. Those from Tondakheiri and Mahddewa are
unbranched, but otherwise agree with those from Kémpti. The stem
(or whatever the columnar body is to be called), is from 7 to 2 inch
broad; along the centre of it runs what we must for convenience
eall the axis, which in the best specimens (from Kdmpti) appears as
a deep narrow channel or furrow, but in some others as a ridge.
This is not straight and even, but more or less flexuous in direction,
and more or less widened out in some parts. From it proceed to each
side in an irregularly alternate order, and at very unequal distances,
what seem to be partitions, dividing the surface of the fossil on each
side of the axis into portions of various lengths. The surface
between these partitions is irregularly prominent or gibbous, and in
most of the specimens shows no decided traces of organic structure.
But in the largest specimen from Kimpti, I observe appearances
which seem clearly to indicate a continuous cellular tissue, as of the
cuticle of a stem or root: the surface exhibits delicate but distinet
longitudinal lines, cross-barred by fainter aud very short transverse
ones; the spaces between being a little raised. The appearance is
exactly that of an epidermis formed of narrow rectangular cells.

1861.] BUNBURY—FOSSIL PLANTS, NAGPUR. 339

The branches are very irregularly alternate ; very often, but not
constantly, they are opposite to one of the supposed partitions; they
are of small diameter in comparison with the body from which they
proceed, but various and irregular in thickness, and not less various
in direction ; in many of them we can trace an axis, like that of the
main body on a small scale. Many of them are again subdivided,
and with a lke irregularity.

Now, this striking irregularity of ramification appears to me to
be very much at variance with the characters of the genus Spheno-
phyllum and the family of Calamitee (or Asterophyllitee) to which
Vertebraria is referred by De Zigno and others. In Sphenophyllum,
Asterophyllites, Annularia, and in those Calamites or Calamodendra
which branch, the branches invariably spring from the articulations
of the main stem, with which they are themselves articulated at
their base; and their arrangement is really symmetrical, though the
symmetry is sometimes disguised by abortion. In this fossil, on the
contrary, the branches are continuous with the main trunk, not
articulated, and are in every way irregular and unsymmetrical. I
conclude, therefore, that the so-called Vertebraria from Kampti is
not a Sphenophyllum, nor one of the Asterophyllitee. On the other
hand, all the characters of the ramification appear to me to favour
the conjecture that these supposed Vertebrarie are roots of some
large plant.

The true original Vertebrarie, according to McCoy, owe their
singular form to densely compacted whorls of leaves surrounding
without interruption a slenderstem. That the supposed Vertebrarie
of Kimpti are not of this nature is rendered evident, not only by
their ramification but also by the character of the cellular structure
observable on the surface of one specimen, which I have already
described.

In the unbranched specimens from the Nagpur district, the indi-
cations of their nature are not so clear; and their appearance might
easily lead to their being classed with the true Vertebrariw. They
seem to me, however, to be in reality of the same nature with the
branched specimens from Kampti. Nor can I at all understand how
distinct (though crowded) whorls of leaves could, in the fossilizing
process, have remained so closely and uniformly pressed together as
to present the appearance of a continuous columnar body through
the whole length of the specimens. In no part of the best of these
pieces can I detect any appearance at all like leaves.

On the whole, then, I am of opinion that the branched specimens
from Kampti, which have been taken for Vertebrariw, were the
roots of some plant, possibly of Phyllotheca; that they had probably
a woody central axis of small diameter; that between this axis and
the outer coat or rind (which probably consisted of loose cellular
tissue) there was a hollow, traversed at irregular distances by in-
complete partitions, which connected the outer coat with the axis.
The unbranched specimens were most likely also fragments of roots,
though this is not quite so clear. The original Vertebrarie, V. In-
dica and V. australis (Sphenophyllum radiatum and S. australe,

340 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

Zigno), must evidently, from the descriptions, be of an entirely
different structure.

13. Kworrta? (Contrer?) Pl. XII. fig. 1.

A single fragment, in a fine-grained red sandstone from Mangali.
This is a cast of a piece of stem or branch, about 3 inch broad, di-
stinctly marked with numerous small, roundish, dot- hike leaf-scars,
arranged with great regularity ina quincuncial or spiral order ; each
scar distant rather more than 1 inch from those nearest to it. No ap-
pearance of definite areole as in Lepidodendron, but a narrow furrow
or crack running down from each leaf-scar for some distance in a
straight line. The form and size of the scars clearly indicate that
the leaves were slender and needle-shaped,

This fragment is perhaps technically referable to Anorria, and
may have belonged to a Lycopodiaceous plant; but its appearance is
so strikingly like that of a small branch of a Spruce-fir stripped of
its leaves, that, in the absence of any positive evidence to the con-
trary, I am strongly inclined to believe it to be Coniferous.

14. Ruizome or a Fern? PI. XII. fig. 2.

A specimen from Méangali, referred (doubtfully) by Mr. Hislop to
Lepidodendron; in a very unsatisfactory state of preservation, but
interesting as having more the look of a genuine Coal-measure fossil
than any other in the collection. Appears to be a small portion of
the surface of a flattened stem, with numerous scars (qu. leaf-
scars?) arranged in somewhat of a spiral or quincuncial order, but
with a good deal of irregularity ; the scars ill-preserved, but seem-
ingly for ming small pits or depressions (as in Stigmaria) of a circular
or transver sely elliptical form, with a small central boss or protube-

vance; the surface between these pits marked with various wavy
transverse wrinkles, which partly enclose the scars, but do not form
definite areola as in Lepidodendron. The appearance is a good deal
like some varieties of the so-called Stigmariw, under which name are
doubtless included the roots of Lepidodendra as well as of Sigilla-
mice. The scars are not, however, arranged with the symmetry
characteristic of Stigymaria. Nevertheless, if well-marked Lepido-
dendra or Sigillarie had been found in the s same beds, I should have
considered it, with little doubt, as a fragment of a root belonging to
one of those families. But as I find nothing else among the Nag-
pur fossils to support such a notion, [am more inclined to conjec-
ture that it may have been a fragment of the rhizome of a Fern.

15. Srem.

Apparently an impression of a large flattened stem, with some-
thing of the appearance of a Sigillaria; but the ribs and furrows
are very irregular, perhaps casual, and of the scars only a few
remain ; these are very small, indeterminate in form and character,
showing a tendency to an arrangement in vertical rows, but not very
distinctly. The specimen is from Silewsda.

LG. rem peel: KUL figs 3.

This specimen is from Silewida, and appears to be an impression

1861. ] BUNBURY—FOSSIL PLANTS, NAGPUR. 341

of a large, broad, flattened stem, without distinct character except
one single, very large, and remarkable scar. This scar is of a
roundish oval form, nearly 13 inch in its greater diameter, and
about 17 inch in its lesser; slightly prominent, and well defined all
round by a slight furrow dividing it from the general flat surface.
It encloses a smaller scar or areola, apparently of corresponding form,
but indistinct in part of its outline; towards the centre there appear
to be some slight tubercles or vascular scars, but very obscure. From
one end (probably the lower) of the large scar, proceeds a kind of
appendage, tapering downward to a point, like the downward pro-
longations of the leaf-scars in Lepidodendron.

This sear, by its general form and appearance, reminds one
somewhat of the leaf-scars of Lepidodendron or of Caulopteris, though
on avery large scale ; but, as there is only one on the whole surface of
this portion of stem (nearly 14 foot long, and in parts 8 inches
broad), it cannot be supposed to be the scar of a leaf. Does it indi-
cate the place of insertion of a disarticulating branch, or of a cone
or some other kind of fructification? I feel at a loss to decide, the
characters being so slight.

The remainder of the surface of this impression is merely marked
with irregular oblique wrinkles.

HG NoUCORTES 7 vo El exellent A

A specimen from Kdmpti, very imperfect, but with much the
appearance of a leaf of an endogen, such as a Yucca or Dracena.
Too incomplete for its length to be determined; but the portion best
preserved is about a foot long, and 2 in. broad in the widest part.
Appears to have been sword-shaped or ribbon-shaped, tapering
gradually towards the apex; the actual point not preserved ; veins
fine, close, simple, and parallel, giving a finely striated appearance
to the surface, with some stronger ones here and there. This last
character seems to show that it is not a leaflet of a Cycad; nor do
I think it was a leaflet of a Palm, for there is no appearance of a
keel or fold along the middle. The base is wanting ; consequently
we do not know how it was inserted on the stem or stalk.

General Remarks on the Fossil Plants from Ndagpur.

1. The first thing that strikes us is the paucity of distinct forms
in proportion to the abundance of specimens. ‘This paucity is even
greater than one usually observes in collections from the paleeozoic
coal-fields of Europe or America, and is strongly contrasted with
the rich variety of forms presented by most of the tertiary plant-
deposits, especially by the miocene formations in Germany and
Switzerland*. Everything points to the conclusion that the plant-
bearing deposits of Nagpur (and seemingly also the others in India
of the same age) were formed in districts which had a limited and
monotonous flora, singularly poor in species, though abundant in
individuals, and very probably luxuriant in growth. It would

* See Goppert on the Fossil Fiora of Schossnitz; Wessel and Weber on the
Brown-Coal of the Rhine; Heer, and others.

342 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

be rash to conclude that such were general characteristics of the
Indian flora in those times. Some might be disposed to account
for this monotony by supposing that the fossil plants of Nagpur
are merely the scanty remaining fragments of a rich vegetation ;
and that the other plants with which they were associated, being less
adapted for preservation, have entirely perished; but it is hardly
possible to admit this explanation when we observe the remark-
able variety of vegetable forms in the tertiary plant-beds, which
must also have been deposited under water. We do not know of
any conditions which would account for the preservation of so many
various forms in the one case, and of so few in the other.

2. Another and very striking characteristic of this Nagpur fossil
flora, is its close analogy with that of the coal-formation of Aus-
tralia*. The prevailing plant in each of the deposits is a Glosso-
pteris, and it appears (as far as we can judge in the present state of
our knowledge) to be actually the very same species in both. My
Glossopteris leptoneura, an abundant plant in the Nappee beds, is
very closely allied to the Australian G Glossopteris linearist. Another
most abundant plant of the Nagpur deposit is a Phyllotheca, a
genus especially characteristic of the Australian coal-formation ; and
the species, though not identical, is very similar to those of New
South Wales. I may add the genus Vertebraria, which, though =
have met with no certain evidence of its occurrence in the Nagpur
district, is known to be common to the Bengal and Australian eal
fieldst. Thus it appears that those vegetable forms which are most
striking by their peculiarities, and most characteristic by their abun-
dance, are common to these two distant countries. At present, as
is well known, the vegetation of extra-tropical New South Wales is
very widely different “from that of continental India. If, indeed,
we compare tropical Australia with India, we find, as Dr. Hocker
has shown§, a very marked agreement between their floras; nearly
200 species being common to the two. These indeed are plants of
very different character from those which occur as fossils in either
country, and afford very different climatic indications; they are the
plants of a dry climate and of open and arid countries ; whereas the
fossil plants must, in all probability, have grown in or near extensive
swamps or large bodies of water. It is however worth observing
that, where the physical conditions of the two countries are nearly
similar, there is at present this marked agreement between their
floras. It is also to be observed that in each of the fossil floras
which we are comparing, the Ferns are the predominant family, and
that the Ferns of Australia at the present day are among the least
peculiar portions of its vegetation. ‘Several species of this family
are common to India and New South Wales; such are Drynaria
trioides, D. quercifolia, Asplenium nidus, Davallia elegans, Cheil-

* See Morris in Strzelecki’s New South Wales; and McCoy in Ann. Nat.
Hist. v. p. 20.

+ And may possibly not be specifically distinct from it.

+ See McCoy w# supra, and De Zigno, Flora Foss. Form. Oolith.

§ Introductory Essay on Flora-of Australia, p. 42.

1861. ] BUNBURY—FOSSIL PLANTS, NAGPUR. 343

anthes tenuifolia, and Gileichenia Hermanni, When, therefore, the
climatic or local conditions were such that the mass of the vegetation
consisted of Ferns, we need not be surprised to find a much greater
agreement than now exists between the two countries.

3. Next, as to the geological indications afforded by these Nagpur
plants. Messrs. Hislop and Hunter consider the age of this deposit as
Oolitic (Jurassic) ; McCoy inclines to the same conclusion with regard
to the coal of New South Wales; and De Zigno, in his writings on
the fossil flora of the Oolite, has without hesitation included under
that category the coal-formations of both India and Australia. On
the other hand, Prof. Jukes (as quoted by Dr. Hooker*) seems to hold
that the coal-formation of Australia is paleozoic. It is very diffi-
cult, looking to the points of agreement I have already enumerated,
to believe that the Indian and Australian fossil floras were far
remoyed in time. If the resemblances between them are not worthy
of confidence, still less then can we trust to the analogies of either
with those of Europe.

The fossil flora of Nagpur is certainly in its general aspect more
like that of the Jurassic than of the Carboniferous age. I do not
find in it, however, any plant which I can determine to be specifically
identical with one belonging to the European Oolite. The Tenio-
pteris (T. dancoides?) from Nagpur is not, perhaps, satisfactorily
distinct from 7. major of the Yorkshire Oolite; but our materials
do not allow us to identify it with that species. The genus Glosso-
pteris, so especially characteristic of the Indian and Australian plant-
beds, contributes much to give to those formations a mesozoic rather
than paleozote aspect, since it is perhaps, as a genus, undistinguish-
able from Sagenopteris, of the Oolite and Keuper, while, on the
other hand, it has little resemblance to any Ferns of the Carboniferous
age. Nevertheless, a certain degree of caution must be observed in
concluding that particular genera of Ferns are absolutely charac-
teristic of particular geological periods. It has been remarked =
that there is a certain analogy or proportion between the geo-
graphical and the geological distribution of organized beings. Now
there are very few instances in which the genera of recent Ferns
have a strictly limited geographical area: searcely any genus
(excepting those which consist of only one or two species) is
confined to a single geographical province or region§. Very many
even of the species of Ferns (as has been amply shown by Sir W.
Hooker and by Dr. Joseph Hooker) have a wide geographical range.
With the genera this holds good in the majority of cases ; and the in-
stances are numberless in which we find nearly allied or representa-
tive species in distant countries. It appears therefore to a certain

* Introductory Essay on Flora of Australia, p. 100, 101.

t By the Zndian fossil flora in this memoir I always mean that of the sup-
posed Jurassic beds of Nagpur, of the Rajmahal Hills, and of the Burdwan
coal-field. By the Australian fossil flora, I mean that of the coal-formation of
New South Wales.

+ By Edward Forbes and others,

§ Seewhat is said on this point by Mr. John Smith, Hooker's Journal of Botany,
vol iv.

344 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 20,

degree probable that the generic forms of Ferns may have had a
wide range in time also, and that allied (though not identical) species
may have existed in very different ages. I do not wish to lay much
stress on this argument; but it may suggest a certain degree of
caution. The genus Phi yllotheca affords more decided evidence of
Jurassic affinities in the fossil flora of the Indian and Australian
coal-fields, since the only known species owt of those coal-fields
have been discovered by M. de Zigno in an undoubtedly Jurassic
formation in Northern Italy*. The other vegetable remains of the
deposit we are considering are too uncertain in their nature and
affinities, or too remote from any known in Europe, to afford any
help towards determining the question of age.

On the other hand, there is in the Nagpur collection a striking
deficiency of the Cycadee (Pterophyllum, Zamites, Otozamites, and
the lke), a family very characteristic of the Jurassic flora in Europe.
This deficiency does not extend to the plant- bearing deposits of Bengal.
Dr. McClelland describes several well-marked Cycadeew from the
Burdwan coal-fields. In a set of drawings, which I have examined,
of fossil plants procured by Prof. Oldham from the Rajmahal Hills,
as many as nine out of thirteen forms represented are undoubted and
well-characterized Cycads. In the Australian coal-fields, again, 1
have no evidence that any Cycads have been found. The question
may therefore arise, are the fossil plants of Nagpur contemporaneous
with those of Australia, and of a different age from the Burdwan
and Rajmahial deposits? But the Glossopteris Browniana appears to
be common to the Australian and Bengal coal-fieldst ; so also is the
very peculiar and characteristic form called Vertebraria. I think,
therefore, that the several plant-bearing deposits of which I have
been speaking, cannot well be separated geologically, and that, as
far as the evidence derived from fossil plants can be trusted f, there is
a strong probability that they are all of Jurassic, or at least of Meso-
zole age.

4. The fossil flora deseribed in this paper appears fully as differ-
ent from the existing vegetation of India, as the fossil flora of our
Jurassic or our Carboniferous rocks is from the existing vegetation
of Europe. Drs. Hooker and Thomson, in their admirable Intro-
duction to the ‘Flora Indica,’ have shown us what are the character-
istic families, genera, and species of plants in the different districts
of India; and in none of these districts do we find anything
resembling the fossil vegetation of Nagpur. ‘The predominance of
Ferns, the absence of any certain indication of ordinary (angio-
spermous) Exogens, the absence of Palms, and, in fact, the apparent
absence of all those families and genera of plants which can be
considered in any way characteristic of the Indian flora, strikingly
distinguish this extinct vegetation from that of the present day. If
it were contemporaneous with our Jurassic flora, it cannot be denied

* De Zigno, Fl. Foss. Form. Ool., pp. 59, 60.
t Brongniart, Hist. Vég. Foss. - McCoy ; Morris in Strzelecki’s New South Wales.

t To what extent evidence of this sort can be trusted must remain doubtful
ata the Petit-Ceur mystery shall be solved.

1861. ] BUNBURY—FOSSIL PLANTS, NAGPUR. 345

that the vegetation of India was in those ages much more similar to
that of Europe than it is now.

The absence of Palms from a deposit representing to us the vege-
tation of an Indian district is the more striking, because both the
leaves and the seeds of those plants are of a very durable nature, and
likely to be preserved. In the Bengal coal-field, indeed, is found a
Zeugophyllites, which Prof. Brongniart appears to consider as an
undoubted Palm; but I can find no trace of it in the Nigpur
collection.

Postscript.—Since this paper was thus far completed, I have received
Professor Oldham’s memoir* on the geological relations of the rocks of
Bengal and Central India, which throws some new and important light
on the subjects I have been discussing. Accordingly I find it necessary
to correct in some points the opinions as to the geological age of
these fossil plants, which I have above expressed. Prof. Oldham
shows that the group of rocks of the Rdjmahdl Hills constitute a
formation quite distinct from that of the coal-bearing beds of Burd-
wan and some other localities ; to which latter group he applies the
name of the Damuda beds. He shows that the fossil vegetation of
the two formations is entirely different, both specifically and in
general aspect ; that not one species is common to the two; that the
Réjmahal beds are characterized by a remarkable abundance and
variety of Cycadee, by a comparative paucity of Ferns, and by the ab-
sence, in particular, of the genus Glossopteris, as well as of Phyllotheca
and Vertebraria; while the Burdwan or Damuda beds are characterized
especially by Glossopteris, Phyllotheca, and Vertebraria, with scarcely
a trace of Cycads. It is evident that the Nagpur fossil flora agrees
altogether in these respects with that of the Damuda, and not with
that of the Rajmahal formation. Prof. Oldham is of opinion that
the Rejmahal beds are mesozove, and probably Jurassic—the Damuda
beds palwozoie. On this latter point I am not entirely prepared to
go along with him. I still think, for the reasons already given, that:
the facies of this Nagpur and Burdwan flora is rather mesozoic.
But this is a pomt by no means clear, and one on which much
further light is yet required before we can come to a safe conclusion.
The paleeobotanical evidence is far from unequivocal, and, such as it
is, might be outweighed by the discovery of a single well-marked
and thoroughly characteristic fish, shell, or coral.

I perceive that Prof. Oldham has come to the same conclusion
touching the so-called Vertebrarie in general at which I had already
arrived in relation to those of the Nagpur collection ; namely, that
they were roots. As he observes, they seem to have played a some-
what similar part, in the Bengal coal-field, to that of the Sagmarie
in the coal-fields of Europe and America.

* Memoirs of the Geological Survey of India, vol. ii. part 2. 1860.

346 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Mar. 20,

DESCRIPTION OF PLATES VIII.-XII.
Puare VIII.

Fig. 1. Glossopteris Browniana, var. Indica, dd. Brongn. An
imperfect frond.
Fig. 2. ————. Apex ofa frond. F ;
di. 3. ————. Base ofa frond. From Silewada.
ig. 4. ————. Enlarged portion of a frond, showing the
venation and sori.
Fig. 5. Glossopteris Browniana, var. Australasica, 4d. Brongn. From the foot
of the Mahidewa Hills.
Fig. 6. Glossopteris muszefolia, C. B. An imperfect frond. From Silewdda.

Puate IX.

Figs, 1-3. Glossopteris leptoneura, C.B. From Kaémpti.
Fig. 4. . Portion of frond, magnified.
Fig. 5. Glossopteris stricta, CB. From Silewadi. Reduced 4th.

Fig. 6. Pecopteris ? :
Fig. 7, ————— b Pay HOO! O asont | From Kampti.
Fig. 8. ————— Enlarged leaflets.

PuaTE X.

Fig. 1. Cladophlebis? Portion of a frond. From Kampti.
Fig. 2. Teeniopteris danzoides (?), McClel/. Portion of a frond. From Kémpti.
Fig. 3. Filicites (Glossopteris?). Imperfect frond. From Silewdda.
Fig. 4. Filicites (Glossopteris?). Imperfect frond. From Kampti.
Fig. 5. Neeggerathia ? (Cyclopteris ? Hislopii, C.B.). Imperfect leaf. From
Bharatwada.
Figs. 6-9. Phyllotheca Indica, C.B. Portions of stems. From Bharatwada,
Silewidé, &e.
Puate XI.
ne ai Phyllotheca Indica, CB. Portions of stems. From Bharatwada,
Fig. 3. Roots of Phyllotheca? From Kampti.
Puate XII.
. Knorria? (Portion of stem of a Conifer ?). From Mangali.
. Stigmaria? (Portion of the rhizome of a Fern ?). From Mangali.
. Portion of a stem with a large scar. From Silewada.
Yuccites ? Imperfect leaf. Reduced. From Kampti.

Fig.
Fig.
Fig.
Fig.

He COLO

2. On the Aan of the Fossrurrerous THin-BEDDED Sanpsrone and
Coat of the Proyixce of NAepur, Inpia. By the Rev. Srepnen

Histor.
(Communicated by the President.)

¥ ConTENTS.
. Nagpur Circle.
. Barkoi and the foot of the Mahadewa Hills.
. Western Bengal. 4. Mangali.
. Kotaé on the Pranhita. 6. Réjmahal Hills.
Comparison of the strata and fossils of Nagpur, Barkoi and the Mahadewa
Hills, Mangali, and Kota.
(1.) Fossil flora of New South Wales.
(2.) Fossils of the Indian Plant-bearing Sandstones and Coal-fields,
A. Plant-remains. B. Animal-remains.

ST OVeo ho

1. Ndégpur Circle.—If with a radius of 14 miles a circle be drawn
around the city of Nagpur, it will include within its northern half
Kampti, Bokhara, Silewida, Tondakheiri, Babulkheda, and Bha-
ratwida; but it will leave out Arajmet, which hes 20 miles west of

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1861.] HISLOP—NAGPUR SANDSTONE AND COAL, 347

Nagpur, and Chorkheiri, which is 35 miles to the north-east, while
Chanda is situated 85 miles to the south. At all these places the
thin-bedded sandstone with vegetable remains is the same, as it pre-
sents the same appearances both paleontological and lithological.

2. Barkoi and Mahdédewa Hills—That this thin-bedded sandstone
is identical with the coal-shale at Little Barkoi, near Umret, and at
the base of the Mahddewa Hills, in the N.N.W. part of Négpur pro-
vince, I have ascertained by personal inspection, and haye endea-
voured to prove in the Quart. Journ. Geol. Soc., vol. x1. p.555, At
all the localities already named, arenaceous as well as carbonaceous,
there is a similar group of fossils; and at Bokhdrda, an acknowledged
site of the plant-sandstone, there is a tendency among the strata,
which are usually white, to become brown and carbonaceous through
the abundance of their comminuted vegetable matter.

3. Western Bengal.—That the plant-sandstone and carbonaceous
beds of Nagpur are of the same age as the coal-strata of Western
Bengal, I have attempted to show in the ‘ Quart. Journ. Geol. Soc.’
loc. cit. The rocks of both provinces have embedded the same flora,
including species of Pecopteris, Glossopteris, and Teniopteris, Verte-
braria Indica*, Trizygia (or Sphenophyllum) speciosa, a species of
Phyllotheca, and a stem, which M°Clelland has erroneously named
Poacites muricata. Many more points of resemblance, I have no
doubt, will be discovered when the Bengal strata shall have been
more carefully examined.

4, Mdngali.—Thus far I may calculate on a general concurrence
in my conclusions; but, when I embrace in this comparison some
thin-bedded, red, argillaceous sandstone at Mangali and Mesa, about
60 miles south of Nagpur, difficulties arise, and a difference of
opinion has been expressed. In a Report on the Talchee Coal-
field, by Messrs. Blanford and Theobald, the authors seem disposed
to place the Mangali beds above the plant-sandstone and coal; and,
as they consider the former Permian, the two latter they regard as
at least of that ager. It must be admitted there is some apparent
ground for this view. The strata within the semicircle north of
Nagpur, and at the other localities mentioned in paragraph 1, are
of a whitish hue; those at Mangali are of a brick-red colour. Jn the
former the fossils, with the exception of an Insect’s wing found at
Kampti, are exclusively vegetable; in the latter they are chiefly
animal. In the one Ferns abound, in the other not one has
hitherto been discovered; but, instead of them, we have the rep-
tilian Brachyops laticeps (Owen), an undescribed species (if not
two) of the crustacean Hstheria, and the jaws and scales of
ganoid Fishes. Yet this distinction in colour and fossil contents
most probably depends on a difference, not of time, but of local
condition ; for, with all the dissimilarity, there are numerous points
of agreement. The strata near Nagpur and Chinda, and those at
Mangali, intermediate between these two places, though differing in

* Vertebraria and Trizygia are not recognized in the preceding paper by Sir
C. Bunbury as occurring in the plant-bearing sandstones of Nagpur.—Eprror.

+ Mem. Geol. Surv. of India, vol. i. pt. 1, p. 82.

348 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

colour, are alike in many other respects. Both are thin-bedded and
argillo-arenaceous, and, after continuing so for about 15 feet, they
both pass into a coarser whitish sandstone below ; and though the
fossils are so diverse in their general character, and though many ve-
getable remains found near Nagpur and Chanda are wanting at Man-
gali, yet the fossil plants that do occur in the latter neighbourhood
are on the whole similar to those in the former. Thus at Mesa there
is a seed or seed-vessel about 2 in. long, and + in. broad, resembling
a paper kite in form. This also occurs of the very same dimensions
and shape at Kampti. Again, a smaller fossil of a similar kind is
common to the beds at Mest and Bharatwada. Further, a small piece
of stem from Mangali, with distant lanceolate scars running along
it, is the miniature of a larger branch from Kémpti. And, lastly,
Méangali furnishes various sulcated jointed stems, which, as far as
the state of their preservation warrants a judgment, resemble stems
abundant at Kampti, Silewada, Bharatwada, &e. This amount of
agreement, apparently specific, between the fossils from Méngali
and from the vicinity of Nagpur, is sufficient, in my opinion, to autho-
rize the inference that the strata contaming them are nearly, if not
exactly, on the same geological horizon.

5. Kotd on the Pranhité.—And now, as I have pointed out the
connexion between our Nagpur plant-strata and those of Bengal, so
with the addition of the Mangali beds and their animal remains, I
may institute a comparison between them and the rocks at Kota, on
the Pranhitd. There, under a great thickness of coarse iron-banded
sandstones, developed in the neighbouring hills, we have thin-bedded
strata abounding, as at Mangali, in animal remains, including
Lepidotus Deccanensis, L. longiceps, L. breviceps, and Gehmodus
figertoni. In addition to these ganoid Fishes obtained by the late
Drs. Walker and Bell, I have procured from the same locality the
exuyie of Insects and Entomostraca, among which there are Cypride
and a species of Estheria determined, on the authority of Mr. Rupert
Jones, to be identical with the larger form at Méngali. With this
connecting link between the two series of rocks, the presumption is
that they are of the same age. The vegetable remains at Kota seem
to consist principally of stems, but in such an imperfect state of pre-
servation as to be wholly unrecognizable. Dr. Bell, however, in a
layer of sandstone only 6 feet below the ichthyolitic bituminous shale,
discovered impressions of “ leaves,’’ which (although he was disposed
to consider them dicotyledonous) belonged to a genus with simple
entire fronds and anastomosing venation; and I conceive myself
justified in believing them to have been acrogenous, and belonging
to a species of Glossopteris. The arenaceous stratum contaiming
them is obviously part of the same series as the bituminous shale,
with which it alternates, there being as much of the shale below as
above the sandstone. Now, as from the existence of a species of
Estheria common to the rocks at Mangali and Kota, we inferred
their contemporaneousness, so from the discovery of what appears to
be a species of Glossopteris at Kota, we are led to the conclusion
that the rocks there are connected in age with those near Nagpur,

1861. | HISLOP—-NAGPUR SANDSTONE AND COAL. 349

in which that genus abounds: and this comparison of the strata at
Kota, first with those at Mangal and then with those near Nagpur,
confirms the evidence which I have already adduced of the close re-
lation between the Mingali and Nagpur beds.

Dr. Bell’s shaft, which has furnished me with most of my infor-
mation regarding the succession of strata at Kota, ended in a deposit
of red clay lying 73 feet below the bituminous shale with Fish-re-
mains. Can this be the red clay which is found at Mdledi, 30 miles
N.N.W. of Kota, to embed coprolites and several forms of Ceratodus
teeth, which have been described by Dr. Oldham in a recent publi-
cation of the Indian Geological Survey ?

6. Rdjmahdl Hills—How the upper beds of the Rajmahal Hills
stand related to the strata that have engaged our attention, and
whether there are any examples of them in the Nagpur province,
are questions which meet us here. It is obvious that some interval
elapsed between the deposition of the inferior and superior beds at
Rajmahdl. How great, then, was that interval? To me it appears
not to exceed the space of time requisite for a whole formation ; as
the floras of the respective periods, though different, are not so di-
stinct as to indicate a decided change in the circumstances of their
growth. In both we have Tanopteris and the Cycadacew, the latter
being represented in the lower strata of Bengal by Zamites Burdwa-
nensis, and in the higher by several species and genera. The equi-
valents of the upper Rajmahal beds have been met with by Mr.
H. B. Medlicott, on the Hurd River, a little south of the Narbadda*.
This discovery brings the existence of these rocks very near our
province, but hitherto they have not been found within its limits.
It is possible that some of the vegetable impressions occurring at
Kampti, especially one or two species of T'ceniopteris, are originally
from this source; for most of the fossil plants there are not found
in situ, but in blocks dispersed through the coarse iron-banded sand-
stone. There can however, I think, be no doubt that the greater
portion of these remains are the same as others still in their original
position in the laminated sandstone of the neighbourhood; and even
to the hypothesis that the remainder may belong to a younger
group of strata, there 1s this objection, though only of a negative
kind, that at Kampti, so far as known, there is a total absence of
the Cycadacee which characterize the upper beds of Rajmahal.

7. Comparison of the Strata and Fossils of Nagpur, Barkoi and the
Mdladewas, Mangah, and Koté.—Setting, then, this higher series at
Rajmahal and the Hurd River in a category by itself, let us endea-
vour, by a comparison with formations out of India, to determine
the age of the rocks near Négpur, at Barkoi and the Mahddewas, in
Western Bengal, and at Mangali and Kota, all of which we have seen
to be almost, if not altogether, contemporaneous.

(1.) Fossil Flora of New South Wales.—There are certain deposits
in New South Wales which, it must be acknowledged, present ob-
vious features of resemblance to the Indian strata under considera-
tion. The connexion between those beds in Australia and ours in

* Indian Records, x. p. 17.

300 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar, 20,

India consists in the occurrence in both of the genus Pecopteris,
Sphenopteris, Glossopteris, Phyllotheca, and Vertebraria; a leaf which
is figured in Strzelecki’s ‘ Physical Description of New South Wales ’
under the name of Zeugophyllites ; and a large seed or seed-vessel, of
which there is an Australian specimen in the British Museum, In
regard to the genus Glossopteris, the resemblance between some of
the specimens from India and others from Australia is so close as to
lead to the belief that the species are either nearly allied or identi-
cal. The same may be said of the genus Vertebraria*, the leaf, and
the seed or seed-vessel aboye referred to; while there is a general
similarity of form in Pecopteris, Sphenopteris, and Phyllotheca. At first
sight the vegetable remains which I have enumerated might be
regarded as paleozoic, seemg they are found in strata which in
Australia are said to alternate with beds containing Mollusks of a
Carboniferous or even Devonian aspect; but as the localities where
these shells occur are far from affording a complete series of forma-
tions for comparison with those of other countries, their precise age
cannot in the mean time be ascertained. The southern hemisphere
seems to be the only part of the world in which we meet with such
a combination of plants and quasi-carboniferous or quasi-devonian
shells; and since in other districts plants similar to most of them
are common, along with animal remains that are evidently not pa-
leeozoic, we are reduced to the necessity of supposing either that shells
apparently palaozoic survived in Australia to mesozoic times, or
that plants which in other places flourished at a comparatively late
period were introduced on the stage of beimg there at an earlier
epoch. Perhaps it will be found that the Mollusks and Plants at
our antipodes met each other half-way ; for while there is a great re-
semblance in the floras ef the Indian and Australian geological fields
which we have been comparing, and while, on the whole, they ex-
hibit a Lower Jurassic facies, yet some plants that are most charac-
teristic of the Jura formation are wanting in New South Wales,
though frequent in India—I refer to Twniopteris and Zamites. But
this is mere conjecture. It must be confessed that the whole sub-
ject of these fossils from the Neweastle and Hawkesbury basins is in-
volved in obscurity. Still that obscurity, resting on isolated spots
with a very limited succession of rocks, ought not to prevent us from
receiving light from other parts of the world, where the stratigra-
phical series is much better developed, and the relations of its various
members indisputably fixed.

(2.) Fossils of the Indian Plant-bearing Sandstones and Coal-
jields.—To the consideration of these better-known localities let us
now proceed.

A. Plant-remains—Among our Indian plants a very marked
feature is the abundance of simple-fronded Ferns. This of itself, as
it appears to me, would favour the supposition that the rocks in
which they occur are of Jurassic age, as it is in strata of that period
that simple-fronded Ferns are most numerous in Europe. But the
inference becomes still more probable when we advert to the parti-
* See the remarks on Ver‘edraria in the preceding paper, svpra p. 339,—Eprr.

1861.] HISLOP—-NAGPUR SANDSTONE AND COAL. 351

cular genera of these Ferns. The most common is Glossopteris. This
is not at present looked on as a European genus; but having had
an opportunity, through the kindness of Professor Allman, of in-
specting the plants collected by the late Hugh Miller at Helmsdale,
and now deposited in the Museum of Edinburgh University, I see
no reason to doubt its occurrence in the Oolite of Sutherlandshire.
Most of the specimens that I examined, I am aware, are probably
only detached portions of the compound frond of Sagenopteris; but
there are others, such as those marked “ 48” and “ 104,’ which seem
too large to beso regarded, Besides, some (¢. g. No. 54) are furnished
with one or two specks that bear a striking resemblance to the
punctiform sori of a true Glossoptercs. At Bayreuth also there are
single fronds, which differ in size and form from Sagenopteris, and
agree much more in these respects with our Indian genus. If,
therefore, the Lower Jura of Bayreuth and the Oolitic beds of Helms-
dale do indeed yield Gilossopteris, then the presumption is that,
seeing this genus, like its nearest ally among the compound-fronded
Ferns, is confined in Europe to the Jura, our eastern rocks contain-
ing it belong also to that formation.

A similar conclusion may be deduced from the abundance in India
of the genus Teniopteris. If all the specimens found in the blocks
at Kampti are from the inferior beds, there would seem to be three
species from these rocks in our province, one of them being from
the carbonaceous strata at Barkoi in situ. Now this genus, with
the exception of two or three species, is never found at a lower level
than the Trias, and it even ranges as high as the Wealden. It
reached its maximum, however, as is well known, in the Jura. One
of the species common in the Kémpti boulders bears the closest affi-
nity in shape, size, and venation to Teniopteris magnifola of Prof.
W. B. Rogers, from the lower Jurassic strata of Eastern Virginia, —

The same relation to European Ferns of Jurassic age is borne by
our compound-fronded genera. One species of Pecopteris from
Kampti seems to me to resemble P. Haiburnensis from the Lower
Oolite of Scarborough, more than any older form. Again, we have
from Kémpti a tripinnate frond with bifurcate venation, but without
a central midrib, which differs from any genus, so far as I know,
that has yet been described. A similar Fern, however, without a
name, has been figured by Baron de Zigno from the Lower Jurassic
beds of Northern Italy.

In the province of Nagpur we have hitherto met with no decided
Cycadacee. But the contemporaneous coal-basin of Rani-ganj, ac-
cording to M°Clelland, presents us with a species which he has
named Zamia Burdwanensis. Few members of this family have
yet been discovered under the Jurassic formation. At Kémpti there
has been found a portion of a leaf, apparently lanceolate, with fifteen
somewhat parallel veins, which in a preceding part of this paper I
have identified with the Zeugophyllites of New South Wales. This
name has been changed by Schimper and Mougeot for Schizoneura ;
but in my opinion the Schizonewra of these authors is not the same as
the leaves of New South Wales and Kdmpti. The plant figured from

VOL, XVII.—PART I, 2B

302 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

the Gres bigarré of the European continent appears to have possessed
narrow leaves arranged in a verticel; but our leaf and that from
Australia are broader, and agree better with the pinne of a plant
from Burdwan, which is now in the British Museum. In that fossil
the pinne resemble those of the larger specimens of Zamites distans,
only they are opposite, and not alternate as in Sternberg’s species.
If I mistake not, its pinne are characterized by 14-16 sub-parallel
veins, like our imperfect specimen. If it is not to be classed with
Zamites, to which it bears an obvious affinity, I think the old name
of Zeugophyllites should be continued for it as the most appropriate.

The stems in our collection present peculiar difficulties. But it is
something to know that none of them belong to the Calamites of
the true Carboniferous series. Those that have been taken for such
appear chiefly to belong to the genus Phyllotheca, which has recently
been discovered by De Zigno in the Lower Oolite of the Venetian
Alps. Iam persuaded that, were the foliage of the sulcated stems
from Eastern Virginia obtained, some of them which agree in all
respects with our leafless stems of Phyllotheca* would be ascer-
tained to belong to this genus, which so abounds in the rocks of New
South Wales, India, and Northern Italy. Another of our stems, not
furrowed however, but ribbed, which was found by my friend Mr.
Hunter at Silewdda, and is distinguished by its deciduous disks near
the joint, is evidently related to the Hgwisetites lateralis from the
Oolite of Scarborough. At Mangali there occur two stems, which, if
I may judge from description alone, resemble two met with in the
Virginian coal-field ; one apparently being a Knorria, and the other
probably having some connexion with the fossil which Sir C. J.
Bunbury compares with Sigillaria or Aspidiaria Menardiy.

In speaking of some reticulated, simple, entire leaves brought to
light by Dr. Bell, I have ventured to suggest that they were most
probably fronds of Ferns, as dicotyledonous leaves of that form are
not known below the Eocene. I am inclined, however, to believe
that exogenous plants did exist at the period in question. At Sile-
wida there is an abundance of stems of considerable size, which have
lost their woody structure, but seem to have possessed bark striated
obliquely upwards from left to right. In addition to this external
marking, most of our specimens exhibit the cicatrices of leaves, and
in one case there is a round sprouting bud left after the foot-stallk
has fallen off. Some of the scars are longitudinal, others are trans-
verse, but all are sparsely distributed over the stem. The transverse
scars slightly resemble those left on the trunk of the Papaw (Carica
Papaya). If the resemblance were to hold good also as to the soft
nature of the wood, we could easily understand how it is that the
trees now referred to present to us nothing but the bark. But,
whether those bearing merely scars are to be ranked as exogens or
not, I must submit, with all deference, that the stem with the round
bud belongs to that division of the vegetable kingdom. And if so,
it would add to the proof whick I have brought forward, that the

* e.g. Calamites planicostatus, Trans. Amer. Geol. Soc. 1840-2.
+ Quart. Journ. Geol. Soc., vol. iii. p. 286.

1861. ] HISLOP—NAGPUR SANDSTONE AND COAL. 358

plant-bearing beds are not very low in the Mesozoic series. These
stems belong to genera seemingly altogether undescribed. The only
fossil that has fallen under my observation which admits of being
compared with them, is one figured by Professor Hitchcock in his
paper on the Sandstone Formation of Connecticut and Massachu-
setts*, which has been shown by Prof. W. B. Rogers to be nearly
on the same horizon as the Richmond coal-basin. The object there
represented, as Sir C. Lyell justly remarks, cannot be a Teniopteris,
but it may very well be a compressed branch or trunk of a tree, on
which supposition the oblique lines from left to right would corre-
spond with the markings on the bark of our Silewdda stems.

Before leaving this part of my subject, I would remark that some
of our seeds or seed-vessels remind me of some that occur in the Lower
Oolite at Stonesfield along with Teniopteris.

B. Animal-remains.—Turning now to the animal-remains, we
find that, like our plants, they are best represented in rocks of the
Mesozoic epoch.

When I transmitted the cranium of Brachyops laticeps to your
Society in 1853, I pointed out its relations to the Labyrinthodontide,
which had never before been recognized in the East, and attempted
also to indicate the section of the family to which it belonged. To
me it seemed to have little connexion with the Archegosaurus, &e.,
but to be allied to that division of Reptiles which Von Meyer has
named Prosthophthalmi, and to approach most nearly the genus Me-
topias. Professor Owen in his description did not enter on this part
of the subject; but I am glad to perceive that Professor Huxley has
since had occasion to allude to it, while speaking of the remains of two
Reptiles from South Africa and Australia, and, without knowing that
it had been done before, has shown a relationship to exist between the
Mangali Brachyops and the Metopias of the Keupert. We are thus
authoritatively furnished with a means of judging of the era of our
Labyrinthodont, which proves to be the division of the Trias nearest
to the Jurassic formation.

Together with the Brachyops skull, there occurs at Mangali a great
abundance of an Hntomostracon, which, in accordance with a sugges-
tion from my friends Drs. Leith and Carter, I was disposed in 1854
to call Limnadia, but which Mr. Rupert Jones prefers to class with
Estheria. 'This species, which is almost equally common at Kota
and Mangali, is somewhat similar to that found in Virginia; but it
perhaps still more nearly resembles in form and ornamentation the
species that sports in the pools of Central India at the present day,
and which a few months ago was described and figured by Dr. Baird
as H. compressat. Besides Estheria we have another genus of Ento-
mostraca at Kota—I mean Cypris. From its elongate form Mr.
Jones feels warranted in saying that, according to our present know-

* Plate 14. fig. 2, Trans. Amer. Geol. Soc. 1840-2.

+ Quart. Journ. Geol. Soc., vol. xv. p. 647. Prof. Huxley here speaks of the
affinity between Micropholis and Metopias, and subsequently of the resemblance
that Micropholis bears to Brachyops.

t Zool. Soc. Proceed., vol. for 1860, p. 188.

2382

304 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

ledge, we should not know where to look for its analogue in rocks
older than the Lower Jura or Upper Trias.

In the same limestone as contains these Entomostraca at Kota, we
are presented with an interesting assortment of Insect exuviee, in-
cluding the wing-covers of Blattide and the elytra of Beetles, which
forcibly remind me of the researches of the Rev. P. B. Brodie in the
Lower Jura of England. The Fishes of this limestone and its asso-
ciated bituminous shale have been pronounced by Sir P. G. Egerton
to belong to a “ true Oolitic form, and apparently of the date of the
Lias*”. Finally, an imperfect bivalve found in the shale with Lepi-
dotus Deccanensis exhibits an appearance of corrugation at the umbo
such as characterizes the genus Unie, a Mollusk of comparatively
recent introduction on the stage of existence.

Combining these results,it would appear that of the rocks which we
have been comparing, while one fossil (viz. the Brachyops of Man-
gali) points to the highest member of the Trias, and while the abun-
dance of Estherie associated with it would indicate either that or
a Lower Jurassic age, the latter organism is found at Kota, with
Fishes, Insects, Cypris, and Unio (?), which are all in favour of an
epoch not lower than the Lias. And to thissame side of the balance
must be added the evidence of Gilossopteris, Teniopteris, a species of
Pecopteris, the furcate-veined tripinnate frond, the Cycadacew, the
Phyllothece, disk-bearing Equisetites, the stems with obliquely striated
bark, and some of our seeds or seed-vessels. It may be that these
Indian strata constitute a sort of passage between the Lias and Trias,
as has been suggested by Mr. Jones in a valuable note on Estheria’ ;
and certainly the Ceratodi of Méledi cannot fail to call to mind the
Bone-bed of Aust; but, upon the whole, I am still of opinion that
the weight of testimony lies on the side of the Lower Jura, as I en-
deayoured to prove in a paper submitted to the Bombay branch of
the Royal Asiatic Society in March 1853. And, on this view of
the age of the contemporaneous fossiliferous strata of Western
Bengal, Nagpur, Méngali, and Kota, if we may assume the red clay
at Maledi to be the same as the red clay in Dr. Bell’s section, about
70 feet below the lowest of the ichthyolitic beds on the banks of the
Pranhita, we may understand how appropriately the Ceratodus teeth
of the one locality are found beneath the Lepidotus, Insects, Hnto-
mostraca, Unio(?), and reticulated fronds of the other.

3. On the Retative Posrrrons of certain PLants in the CoAL-BEARING
Beps of AUSTRALIA.

By the Rev. W. B. Crarxs, M.A., F.G.S.

In the “ Observations on the Flora of the Oolite,” by Baron de
Zigno, published in the Quarterly Journal of the Society, No. 62,

* Quart. Journ. Geol. Soc., vol. vii. p. 272; vol. ix. p. 351.
t Quart. Journ. Geol. Soc., vol. xii. p. 376.

1861.] CLARKE—COAL-FORMATION OF AUSTRALTA. 355

there is a paragraph* respecting the supposed non-verification of
certain genera of plants in the Australian coal-fields, which were
reported by me in 1847.

it is only right that I should offer a few words of comment on
that paragraph.

By reference to the same number of the Quarterly Journal (p. 147),
it will be seen that Mr. Selwyn has already recognized in Eastern
Victoria “true Carboniferous plants;” and he further states that
“in Tasmania the coal-bearing beds rest quite conformably on and
pass downwards into calcareous beds, the fossils from which are, I
believe, nearly all Carboniferous or Devonian forms.”

Now this is precisely the case in New South Wales, in which
colony the plants said to be Jurassic occur (coal-cliffs, Mulubimba,
near Newcastle, mouth of Hunter River) in the same beds and
blocks with heterocercal Fishes, one of which is figured by Dana
as Urosthenes australis, and was acknowledged by Agassiz to be
a paleeozoic fish.

In other portions of New South Wales, and in the new colony of
Queensland, in close connexion with calcareous beds holding abun-
dance of ‘‘ Carboniferous and Devonian” zoological forms, occur
shales and fine calcareous grits charged with the plants which I
reported in 1847, and which Baron de Zigno does not find verified
by Messrs. Morris and McCoy.

The latter gentleman examined and reported on the collections
which I forwarded to Professor Sedgwick, and which are now depo-
sited in the Woodwardian Museum at Cambridge; but he did not
mention the fossils alluded to by De Zigno, because I did not, at that
time, include them in my collections for the university. Nor could
Professor Morris mention such in his account of the fossil flora
published in Strzelecki’s work, because at that time none of the older
forms had been found by Count Strzelecki, and no one besides my-
self had made any discovery of such plants in Australia. But Mr.
Selwyn’s paper referred to above is sufficient to verify the facts I
communicated, so far as concerns the particular genera to which Mr.
Selwyn alludes. Moreover, I placed years ago, in the Australian
Museum at Sydney, specimens of these disputed plants; and in the
present year I saw one of them in the University Museum at Mel-
bourn, which had been found in Gipp’s Land.

Some years since I forwarded specimens to England, and one was
considered at the time, by Professor McCoy, to be a Lepidodendron
of the English coal-fields, so much did it resemble a well-known

* “This would not be the case with those of Australia, if the observations
made in 1847 by the Rev. Mr. Clarke were confirmed; for he mentions in these
deposits the presence of the genera Sigillaria, Lepidodendron, and Stigmaria,
which would settle the question. But I am not aware that the facts thus cited
have been since verified. On the contrary, no mention is made of these genera
in the works of Messrs. Morris and McCoy, in which we are presented with a
series of forms among which, together with local types analogous to those of
India, ner are species which recall the Jurassic flora of Scarborough.” (Vol.
xvi. p. 111.)

t Geolog. U. 8. Soc Expi. Exp., pl. 1. fig. 1.

356 PROCEEDINGS OF THE GEOLOGICAL socreTy. [ Mar. 20,

species. Afterwards another was noticed by the late E. Forbes*, who
expressed his doubts whether that fossil was a Lepidodendron at all.
The late Mr. Stutchbury mentions two from the coal-formation on
the Storton River, in the vicinity of calcareous rocks which have
their equivalents on the Hunter River, where the overlying coal-
measures contain the Jurassic (?) forms. And he also figures one
under the impression that it had not before been figured from
Australia?.

In the course of my explorations in the northern districts of this
colony, I found abundance of these Lepidodendra, with other allied
genera, in a peculiar shale mentioned by the late Allan Cunningham
as occurring on the Peel River t+. This rock occurs also not far from
Goonoogoonoo ; and from it I have made a considerable collection, of
which I now propose to forward specimens for comparison§$ ; as they
resemble in some respects Goppert’s Pachyphlecus || rather than the
usual forms of Lepidodendra, it may be well to ascertain whether
they belong to that plant. Similar fossils exist in the neighbourhood
of Wellington Valley, to the west of Bathurst; and lately I have
found that abundance of them occur in the shale forming the surface
in places, at Canoona (where a considerable gold-field exists), on the
Fitzroy or Lower Mackenzie River in Queensland, nearly half a
degree north of the tropic of capricorn, and a few miles east of the
150th meridian. They were considered by the persons who first
saw them there as belonging to a ‘“ tesselated pavement,” and ex-
cited great curiosity. In one of the grooves defining the leaf-
scars, I detected a minute particle of gold, which had settled in it
from the alluvium above.

M. Odernheimer also mentions similar Lepidodendra in his
account of the Peel River district, published im our Proceedings { ;
and from my own inquiries I know they occur abundantly along the
Manilla River, and in that part of the Liverpool Plain country which
skirts the western limits of the Peel and Bingera Gold-fields, the
latter of which has on that border coal (near Warialda), and just
such grits and sandstones as cover the coal along the coast from the
Hunter to the Illawarra; the usual underlying calcareous beds,
abounding in Carboniferous and Devonian zoological forms, also
making their appearance, as they do to the west of Newcastle.

I consider, therefore, that there has been a sufficient verification
of some of the genera I reported in 1847 **, since they have thus
been found in various parts of a region extending from 23° to 37°
S. lat., at least one thousand miles of direct distance.

Tn the collection which I exhibited at Paris in the year 1855, were
included two specimens marked in the catalogue as “ Lepidoden-

* Lectures on Gold, 2nd edit. p. 53.
+ Report to New South Wales Government July, 1853; Parliamentary Blue
Book, Dee. 1854, p. 18—20.
+ Proceedings Geol. Soc., vol. ii. p. 109.
§ The specimens have not yet arrived, July 15, 1861.—Eprr.
| Fossilen Farnkrauter, pl. 43.
€| Quart. Journ. Geol. Soc., vol. xi. p. 401.
** See also Quart. Journ. Geol. Soc., vol. iv. p. 60.

1861.] CLARKE—COAL-~FORMATION OF AUSTRALIA. 357

dron”’ and one “ Sigillaria*,” and mention is made of the probable
age of them in the introduction to the catalogue of my collection 7.

It cannot, then, be said that publicity has not been given to at
least some of the genera I reported; and if in any of the others I
may have erred from want of means of comparison in this country,
yet there is no doubt that plants apparently older than those called
** Jurassic’ occur in Australia under circumstances no way distin-
guished from those which mark the reputed younger forms, in rela-
tion to the overlying sandstones and underlying calcareous beds
containing true ‘‘ Carboniferous” animal remains.

When Mr. McCoy wrote his valuable account of my fossils at
Cambridge, he concluded from what he saw that there must be two
periods of wide interval—the plants marking an Oolitic and the
animals a Lower Carboniferous epoch, equivalent to that of Ireland,
and without any confusion of typet. But discovering plants of the
genera I reported occurring under the circumstances described above,
and not comprehending how this could be without assuming the
whole series in which coal occurs to be one consecutively, he expressed
the desire that geologists would withhold their judgment till the whole
evidence had been adduced. To assist in this inquiry into the true
age of our Australian coal-beds, I therefore divided the succession of
beds, as in the Paris catalogue before mentioned, and have since
briefly described my divisions in a little work recently published at
Sydney §. These divisions conveniently group the strata, even if,
eventually, they have no direct bearing on epochal succession, though
there really appears to be a sort of grouping in the fossils equivalent
to that in the strata themselves.

It must, however, be observed that the distinguishing feature of
the strata in Australia is their variableness; and to so great a
degree is that observable, that I, for one, would scarcely venture in
any part of the coal-fields to trust any stratum further than I could
see it.

Notwithstanding this, however, there are four main groups of
strata, generally sufficiently distinct for such divisions as I have
made, and which show that it is scarcely right to class them, as has
been done, in two widely distinct formations.

The evidence now collecting as to the formations in other countries
seems also to show that, so far as they are concerned, but little ight
is thrown on the age of the Australian coal-beds; for if, as Baron de
Zigno maintains||, the Richmond plants, and, as Mr. Bunbury says 4],
the Indian plants do not prove what has been deduced from them, so
it may come to pass that the evidence hitherto derived from the
uae flora may, on further examination, receive a modified

orm.

At present no notice has been taken as to the association of

* See British Catalogue Expos. Universelle 1855, p. 102.

t Ibid., p. 100, and P. 8. p. 103.

~ Ann. Nat. Hist., vol. xx.

§ Researches in the Southern Gold-fields of New South Wales, chap. xiv.
|| Quart. Journ. Geol. Soc., No. 62, p. 112. q Lbid. p. 115.

358 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Mar, 20,

certain Fishes with the so-called Jurassic plants; for the fact that a
paleeozoic Fish was found in one of the pits at Newcastle in the
same block with the Plants in question, which are called Oolitic, has
not shaken faith in the latter assumption. Yet that fact must be
explained away before the view in question ought to be adopted.

And if it should be found that certain genera, such as Glossopteris
and Sagenopteris, are not always of so recent date as the Jurassic
epochs ; if it should also be found that the supposed paleeozoic plants
(Lepidodendra, &c.) ascend higher than the Lower or Upper “ Carbo-
niferous,” then it may be that (which I have been inclined to believe
may be the case) there is an epochal as well as stratigraphical suc-
cession in the Australian coal-bearing beds. The only way to settle
the doubt unmistakeably would be to have a complete and careful
measurement made of all the beds supposed to be contemporaneous
in all the Australian colonies, and to collocate them after due inves-
tigation.

But that is at present an ‘impossible quantity; we must be
content with such evidence as we have; and as a contribution to
the general data, I will make a few further remarks.

In Victoria, the geological survey obtained in the early part of
this year a Twniopteris from the neighbourhood of Cape Paterson,
and have recently obtained other plants of supposed like age from
the neighbourhood of Geelong. These fresh discoveries have been
taken to demonstrate the Oolitic age of that vicinity. Now, in my
examination of the Barrabool Hills, near Geelong, in 1856, I saw
enough to induce me to consider that the beds of that neighbour-
hood (especially about Ceres) belong to the first or upper divi-
sion of the New South Wales series, and to my Wianamatta beds.
But the other divisions must not be forgotten. The four divisions
are—l. Wianamatta Beds; 2. Hawkesbury Rocks; 3. (Workable)
Coal-beds; 4. “ Lower Carboniferous Rocks” of McCoy :—

(1. Wianamatta Beds. Upper Carboniferous. 800 | q,,6.
| to 1000 feet thick. PP

“ Jurassic” j; 2. Hawkesbury Rocks (“‘Sydney Sandstone” of Dana). Caves
(McCoy). - Permian
Middle (D an. a)
3. Coal-seams of Newcastle, &c. ; Carboni- :
L | ferous.

x (MeCop) eo \ 4, Lower Carboniferous Rocks.
oy). |
In New South Wales the Wianamatta beds contain Fishes, which
are heterocercal and certainly not so near to Pholidophorus as to
Paleoniscus, to which I consider some of them to belong. A species
of Phyllotheca, as well as Sphenopteris, is found in the same beds
with the Fishes; and a Mytiloid shell accompanies them.
The following Plants from this division I sent to Cambridge, and
they were determined by Mr. McCoy :—
Gleichenites odontopteroides. Pecopteris tenuifolia.
Odontopteris microphylla. { a
[Phyllotheca Hookeri is marked in the memoir from Clarke’s Hill; but it is a
mistake probably from accident, as that species belongs to much lower beds than
these. |

1861.] CLARKE—COAL-FORMATION OF AUSTRALIA. 359

I have recently procured a species, with Fish, from the same divi-
sion, which in some respects resembles a Tceniopteris, but is probably
not such. It will be forwarded to England. In Tasmania, both in
1856 and in 1860, I examined carefully the section from Launceston
to Hobart Town, right through the island, and traced what I believe
to be an equivalent of my Wianamatta beds of New South Wales,
from the neighbourhood of Spring Hill nearly to the Derwent. They
appear to be in great force about Green Ponds and up to Lovely
Banks, near which I found beds before unnoticed as fossiliferous, in
which are plants of a different character to any hitherto found in
that or this country. I will also forward them.

The second division, or Hawkesbury Rocks, are in Strzelecki’s
book classed as Pliocene*; but the Fishes contained in them are
nearer to Platysomus and Pygopterus than to any Tertiary genera;
and over them the Wianamatta beds attain a thickness of from 800 to
1000 feet. No Plants from these rocks were sent to Cambridge,
because I had not then found any. But in the beds with the Fish
were Sphenopteris, &c., and in the massive sandstones, along the
Hawkesbury itself, I have found casts of large fronds like Odonto-
pteris. Neither in Victoria nor in Tasmania have I seen any beds
which I can consider the direct equivalents of these, either in mass
or in distinct resemblance; but patches of sandstone underlying the
supposed Wianamatta beds, about the descent to Bagdad and Brighton,
occur in Tasmania, which might occupy their position. As Mr.
McCoy considers these two divisions with the third, or the work-
able coal-beds, to belong to the Oolite, it becomes important that the
new fossils should be examined. But Mr. Dana considers + that these
same three divisions belong to the true “‘ Upper Carboniferous or
partly Permian.” I have already alluded to the Fish Uvrosthenes
australis, on which in part, as well as on certain Plants, as Negge-
rathia elongata, Mr. Dana founded his opinion.

The Plants from the third division (which cannot be separated from
the second, as the Hawkesbury Rocks cover and pass into the coal-
measures, containing coal-seams in their lowest masses) are, as indi-
cated by Professor McCoy’s memoir, as follows :—

Sphenophyllum (Vertebraria) australe. Glossopteris linearis.

Sphenopteris lobifolia, Morrzs. Neeggerathia (Zeugophyllites) elongata,
alata, 1 var. exilis, Morris. Morris.
hastata. Phyllotheca australis, Brongn.
Germana. ramosa.

—— plumosa. Hookeri.
flexuosa. Otopteris ovata.

Glossopteris Browniana, Brongn. Cyclopteris angustifolia.

The other plants described by Professors Morris and Dana belong
to this division +.

* p. 129. + Geol. U. S. Explor. Exped., p. 495.

t The following are the plants enumerated by Morris :—

Sphenopteris lobifolia. _ Pecopteris odontopteroides,
alata, var. exilis. Zeugophyllites elongatus,
Glossopteris Browniana, Brongn. Phyllotheca australis, Brongn,
Pecopteris australis.

360 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

Thus far, it may be said the evidence went up to a certain period.
But no place has been found for the plants whose verification was
doubted. Where do they belong in Prof. McCoy’s gap between the
Oolite and the “‘ Lower Carboniferous” ?

It might be said truly they are “‘ Upper Carboniferous.” But in
1859 a discovery was made at Stone Creek near Maitland, which
again complicates the question. Mr. Bourne Russell made two pits
at the place mentioned, and passed through four or five workable
seams, the beds between which and on the top, consisting of coarse
grits and conglomerates full of Pachydomi, Spiriferi, Orthoceratites,
large Conularie, Asteride, &c., prove that these coal-seams are not
in beds supposed to be Oolitic, but in McCoy’s Lower Carbonife-
rous. And to complicate still further the whole, below the coal-
seams a bed of shale was reached in which are impressions of
Neggerathia (or Zeugophyllites), Glossopteris (or Sagenopteris), and
other plants, such as Cyclopteris, that look as much like Jurassic as
any that are so called.

Mr. Russell, at my request, placed at my disposal the whole series
of excellent specimens, with memoranda of depth, &c. The locality
is known to me, and I collected Pachydomi, &c., abundantly from
the vicinity; so that these seams and Plants unquestionably occur
in the midst of beds considered to be Lower Carboniferous.

I do not pretend to explain this anomaly, if it be one: but it is
deserving of notice that the supposed Lepidodendra, &c., do not
occur in the same beds with the Glossopteris, &c., described by Mr.
McCoy, but they occur apparently in similar relation to the animal
remains in other parts of the country. And they may, for any-
thing known to the contrary, occupy a corresponding position in re-
lation to the lower members of the ‘“‘ Lower Carboniferous” rocks as
the supposed “ Jurassic” plants do to the upper members of that
formation. The whole affair is mysterious, and leads to an opinion
that the hitherto received conclusion must be modified.

Within the last few years the search for coal has been greatly on
the increase in New South Wales ; and various deep shafts have been
sunk between the back of the cliffs at Newcastle and the junction of
the Hunter and Williams Rivers, near which at Muree (Raymond
Terrace) many of the animal remains described by McCoy, Dana,
and Morris were found. Some of these shafts show an uninter-
rupted series of coal-measures to a depth of 400 feet, without
reaching the floor of the basin. Coupled with the facts already
enumerated and divers others, such as the occurrence of coal and

By Dana :—
Conifer. Glossopteris (?) cordata.
Neggerathia spatulata. linearis, Me Coy.
media. Phyllotheca australis, Brongn.
elongata, Morvvs. Clasteria australis.
Sphenopteris lobifolia, Morris. Anarthrocanna australis.
Glossopteris Browniana, Brongn. Cystoseirites (?).
ampla. Austrella rigida.
Reticulum. Confervites (?) tenella.
elongata.

1861.] CLARKE—COAL-FORMATION OF AUSTRALIA. 361

fossilized wood in the midst of the Muree fossils,—the existence of
coal in association with beds of fossils of Lower Carboniferous age on
the Page River, as at Coyeo and at the back of Mount Wingen,
where the coal-beds (on fire) contain plants equivalent to those of
Mulubimba, and appear to be lower than the Spirifer-bearing beds
on the ranges above them,—the occurrence of similar phenomena as
to the presence of the fossilized wood both in the Glossopteris-beds
of Mount Keera and in the Spirifer-beds of Black Head, and others
elsewhere—it does clearly appear that, in the present state of our
knowledge of the stratigraphical disposition in New South Wales, it
is impossible, without a grave doubt, to admit that the whole of our
coal-measures, if any, are of Oolitic age. A more likely solution
of the difficulty would be the adoption of the conclusion that either
the plants are not necessarily “ Oolitic,” or, if some of them
are, there is a descending order of an epochal, as well as succes-
sional kind, which may fill up the gap assumed in theory, by suffi-
cient evidence to remove the difficulty there is to all in receiving it as
satisfactory.

That the Carboniferous formation in Australia, whatever becomes
of the disputed beds, is of very great thickness, may be conceived
from the fact determined by me when I was in Tasmania last March,
that the “siliceous breccia” of Strzelecki* is a member of this
formation. Mr. Gould, the accomplished director of the Geological
Survey of Tasmania, will, it is to be hoped, very shortly furnish us
with certain data respecting some of the points discussed above.

As much of the coal of the southern part of Tasmania is chiefly
anthracite, it would be interesting to show whether it is older than
the seams of Jerusalem, Richmond, Jericho, Fingal, the Mersey, &c.,
and if any phytological evidence exists for connecting it with the age
of the Lepidodendra, &c., of New South Wales; whether all the
coal in Tasmania is younger than the whole of the ‘‘ Carboniferous”
beds with animal remains; whether the coal of the Mersey is con-
nected with the latter in the same way as the coal is at Stony Creek
near Maitland, or is rather related to the coal of the Tertiary deposits
near Launceston.

Tf it is the case that in India genera of plants stereotyped as
‘¢ Jurassic ” are found in varying species in other formations besides ;
if the identity asserted for such plants in distant countries, such as
India and Yorkshire, is disproved—if the Richmond plants are now
acknowledged to be older—if the reputed age of certain plants in
Africa is in the same category,—it may, perhaps, be yet proved that
the assumption of the “ Oolitic” era for that of the Australian coal
is also too general a deduction conjointly from such facts as we have
and from the want of more, especially such as the want of good
unmistakeable deposits in which the animal remains will leave no
further room for doubt. Beyond two specimens found in the super-
ficial Tertiary gravel at Melbourn, no one has pretended to have
discovered in situ any shell or other animal remains of Oolitic age

TEAL, Gy, stay 2,

362 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Mar. 20,

in all Australia*. Loose on the surface in the neighbourhood. of
Grafton, on the Clarence River, a portion of an Ammonite was also
picked up and brought to me; but it may have been dropped by an
emigrant from Hurope, and is of no value in so important a question.

Different, however, is the testimony of my late friend Leichhardt,
who was both a good botanist and a good geologist, and who left
with me his MS. journal, in German, of a geological excursion to
the northward in the year 1842. He therein mentions that he -
obtained a plant (named by him, doubtfully at the time, “ Hguisetum
obtuse striatum?” but which was afterwards found to be a Phyllo-
theca) from one of the lowest beds in the section at Harper’s Hill,
so well known for its abundant ‘‘ Lower Carboniferous” animal
forms; and he further says that he considers that bed was equivalent
to one of the beds in the cliff at Newcastle. There is no doubt
that that plant was in the midst of, and far below, shells and other
fossils respecting which there is no dispute. It is, in short, a fact
well agreeing with the evidence from Stony Creek.

In venturing on this extended discussion of a difficulty, my chief
object has been to show that the age of the Australian coal-beds is
not sufficiently determined at present to justify their being used as a
test of ‘‘ Jurassic” age cf coal-beds in other countries.

At the same time I may add how much I have been gratified in
obtaining Baron de Zigno’s work, and that, notwithstanding all I
have written, I am open to the conviction of evidence.

4. Prof. Huxtry, Sec.G.8., made the following observations on
some Reptilian Remains from North-western Bengal :—Some bones,
found by Mr. Blanford in the uppermost portion of the ‘ Lower
Damuda” group of strata in the Ranigunj coal-field, and forwarded
to Prof. Huxley by Dr. Oldham, have proved to belong to Labyrin-
thodont Amphibia and Dicynodont Reptiles,—hereby affording new
and interesting links with the fossil fauna of the Karoo Beds of
South Africa, and largely increasing the probability that the rocks in
which they were found are of Triassic age.

Notes on some further Discoveries of Frnt ImptemEnts in Beds of
Post-Prrocene Graver and Chay ; with a few Suggestions for Search
elsewhere. By Josepn Prestwicu, Esq., F.R.S., Treas.G.S.

[This paper, read on May 8th, is, by order of the Council, printed in the
August No. of the Journal, that it may be as useful as possible to geologists
during their autumn excursions. |

Smyvc— my communication to the Royal Society+ on the discovery

of Flint Implements in post-pliocene beds at Abbeville, Amiens,

and Hoxne, similar implements have been found in a few new lo-

* Fossils of Upper Mesozoic age have been brought to England from Western
Australia by Mr. F. T. Gregory, and noticed in his paper read before the Geolo-
gical Society on May 22, 1861.—Ebrr.

+ Phil. Trans. for 1860, p. 277.

1861.] PRESTWICH—FOSSIL FLINT IMPLEMENTS. 363

ealities in this countryjas well as abroad. It is not my object at pre-
sent to enter into a full account of these additional discoveries, or
to touch upon the many and tempting theoretical considerations
which suggest themselves, but which yet require further and more
varied data. It is for these reasons that I limit myself to a brief stra-
tigraphical description of these localities, for the purpose of directing
attention to them before our Session closes, and also to suggest a
few other localities where search should be made, in the hope that
during the ensuing summer other members of the Society, who may
have the opportunity of visiting some of these places, may join in the
search and discover fresh facts to throw additional hght upon this
interesting inquiry.

Suffolk.—tIn the course of the summer of 1860 Mr. Warren, an
antiquary residing at Ixworth, near Bury St. Edmonds, searching for
Roman antiquities at Icklingham, between that town and Mildenhall,
received from one of the workmen a peculiarly worked flint imple-
ment. The man told him he found it at a depth of 4 feet, in digging
the gravel at Rampart Hill. Shortly afterwards Mr. Warren in
looking over a heap of gravel by the road-side in that neighbourhood,
found another specimen 5 inches long and of similar form. He
communicated the discovery to Mr. Evans, and this gentleman and
myself took an early opportunity of visiting the place. In descend=
ing the valley of the River Lark, below Bury St. Edmonds, we
traced, at a level a little above the river, a nearly continuous bank
of gravel. At Flempton I discovered in this gravel a small frag-
ment of some mammalian bone*, but neither there nor elsewhere
did we meet with any flint implements. The gravel is composed
chiefly of sub-angular flints in an ochreous sandy matrix. Mixed
with it are a considerable number of siliceous pebbles from the con-
glomerate beds of the New Red Sandstone, with pebbles of the older
rocks, and fragments derived from the boulder-clay, than which, both
from its position and these mineral contents, I believe it to be newer.
It is spread out in rough irregular beds interstratified with seams of
sand. We could find no shells. The following section (fig. 1) shows
the relation of this gravel, a, to the valley and to the boulder-clay.

Although the two specimens in Mr. Warren’s collection want
more conclusive evidence as to their original position, yet neither
Mr. Evans nor I feel much doubt of their derivation from true drift-
gravels; for in shape, staining, and condition they agree precisely
with the flint implements of the valley of the Somme. The Ickling-
ham gravels should now be the object of a careful and long-con-
tinued search. This is the-second locality where flint implements
have been found in Suffolk; Hoxne being situated in the north-east
part of the county adjacent to Norfolk and in the valley of the
Waveney, which runs into the German Ocean. Icklingham, on the
contrary, is within a short distance of Cambridgeshire, and in the
valley of the Lark, flowing into the Ouse, which empties itself into
the Wash at Lynn.

* Teeth of the Hlephas primigenius are found in the gravel elsewhere in the
neighbourhood of Bury St. Edmonds.

[May 8,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

364

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1861.] PRESTWICH—FOSSIL FLINT IMPLEMENTS. 365

Kent.—In August last year Mr. T. Leech, while searching for
fossils in the cliffs between Herne Bay and the Reculvers, ac-
cidentally found in the shingle at the foot of the cliff a well-formed
flint implement. This induced him to make further search, and in
the course of the few weeks he spent there he found altogether
Six specimens. ‘They are all of the spear-head pattern, so common
at Amiens. One specimen, however, is peculiar, and so far unique ;
it is a pointed implement formed out of large, smooth, egg-shaped ter-
tiary flint-pebble. One end of the pebble is brought to a sharp point,
and the other retains its smooth, rounded surface. In February last
Mr. Evans and I, accompanied by Mr. Leech, visited the place, and after
a search of some hours, Mr. Evans found two, and I found one well-
made and undoubted specimen. They were lying on the sand and
shingle at a distance of from 20 to 30 feet from the foot of the cliff,
and distant three-quarters of a mile west from the Reculvers, and a
little to the eastward of Old Haven coastguard-station*. We searched
the chff for them wm situ, but without suecess. It is to be hoped
that the upper part of the cliff—the part to be searched—may
prove more accessible during the summer months. I satisfied my-
self, however, so far as to determine that at that spot there is at
the top of the cliff, which consists in its lower part of the Thanet
sands and Woolwich seriesf, a local pebbly clay deposit of small
extent and about 8 feet thick, and which, I have reason to believe, is
of fresh-water origin, as it closely resembles the fossiliferous deposit
next mentioned. It is to this bed that I would refer the flint im-
plements. Its height above the sea-level is about 50 feet. The
annexed section fig. 2 shows the relation of this bed, a, to the sea-
level, and to the presumed older gravels, 6, which cap the higher
ground.

A few years since I found,in a section at Swalecliff near Whitstable,
a freshwater deposit (a in the western part of fig. 2), overlying the
London clay, and aboundingin land- and marsh-shells, with which were
associated a few mammalian bones. I again visited the spot on my
return from Abbeville in 1859, in the hope of finding flint implements.
My search, however, was not successful. We now again returned to
this spot to make a further investigation. On this occasion we had no
sooner reached the small bay east of the cliff, than Mr. Evans was
fortunate enough to find, lying on the shore, an oval-shaped flint
implement, identical in form with those so common at Abbeville.
The specimen was further interesting from its deep discoloration.
It possesses that bright light-brown colour which characterizes the
specimens from the gravel of Moulin Quignon. We searched the
cliff for specimens in situ, but did not succeed in finding any. We
noticed, however, that the fossiliferous clay was underlain by a bed
of gravel, the flints in which had the same peculiar brown colour as

* An old wooden spout projecting from the upper part of the cliff may at
present serve as a guide to the spot.

+ For the general section of this part of the coast see my paper in the Journal,
vol. viii. pt. xv. p. 264.

366 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 8,

the flint implement. On a subsequent visit, Mr. Evans found a
small fragment of the tooth of elephant in this gravel high up in the
cliff. This freshwater bed forms one of a series which, commencing
at Chislet* near Grove Ferry, where the deposit contains the Cyrena
flueminals with other fresh-water and also some few marine fossils,
seems to fringe, at intervals, this range of hills. This particular
deposit at Swalecliff, although consisting of tenacious clay with an
interstratified bed of sand and of gravel, is more analogous to the
loess in its organic remains than to the Wear Farm deposit; for
hitherto, although the Pupa marginata and Succinea oblonga are
extremely abundant, and a small Helix is not rare, yet I have not been
able to obtain a single truly aquatic shell. The relation of these
beds to the boulder-clay is not here shown.

Bedfordshire.—Another important and better-observed discovery
_ has just been made near Bedford, by Mr. James Wyatt, F.G.8. A few
years since, a remarkable number of the bones of the Elephant, Rhino-—
ceros, Hippopotamus, Ox, Horse, and Deer were discovered in cutting
through a bank of gravel about one mile north of Bedford on the
Great Northern line of railway?. Mr. Evans and I shortly after-
wards, accompanied by Mr. Wyatt, visited this and other sections of
gravel near Bedford. ‘The following year Mr. Evans discovered in
the large gravel-pit at Biddenham, two miles W.N.W. from Bedford,
both Jand- and freshwater-shells at a depth of 8 feet from the sur-
face. These circumstances, combined with the experience acquired
by a visit to Amiens in the autumn of 1860, induced Mr. Wyatt to
turn his particular attention to this pit, which has since been to him
the object of almost a daily pilgrimage. After a search, continued
for many months, he has at last been rewarded by finding two well-
formed flint implements, one of the spear-head shape and the other
oval,—counterparts, in fact, of the two chief French types. The men
had been digging deeper than usual, and it was in a heap of gravel
just thrown out from a depth of about 13 feet that Mr. Wyatt found
on the same day both specimens. A lettert from that gentleman
gives the details of his interesting discovery. I have since visited
the pit in company with Sir Charles Lyell, Mr. Evans, and Mr. Wyatt.
It is situated on slightly rising ground, about 30 to 35 feet above the
level of the adjacent River Ouse (fig. 3). It happens that there is an
old well in this pit, the sill of which is about 7 feet below the former
level of the ground. Jascertained the level of the water to be 21 feet
9 inches below the sill. This therefore gives us 29 feet from the
top of the ground; and if we add, say one foot, for the fall of the
water-line to the river, we have 30 feet as the height here of the
top of the gravel a above the level of the river. The following is

* See another paper by the author, in the Journal of the Society, vol. xi. p. 111.

t A very large quantity of the bones were collected by Mr. Reade ; but unfor-
ey no systematic search was made, and, with this exception, no collection
formed.

+ It is not now necessary to publish this letter, as it is embodied in a communi-
cation (to which I beg to refer the reader), by Mr. Wyatt, to the ‘Geologist’ of June,
in which the sections used in illustration of this paper and other particulars are
reproduced.

1861. ] PRESTWICH—FOSSIL FLINT IMPLEMENTS. 367

the section at that part of the pit where the implements were
found :—

ft. in.

Gepbartheand sravellyssoill i). tsuneo chee + © « dele s Jey)
6. Coarse light-coloured gravel, upper part irregularly stained

brown with apparently infiltrated clay ......... ase ONL GT

¢. White and yellow sand, with Zimneus .........2..4.. 1 8

Cama Waltidishigtine ora viele. (eteieyat us) si shrpeadlia o'clev a) oh eile eho e Lee)
e. Seam of ochreous sand and grey clay, with Helivw and

JRGRIDEUS 05 S16 O86 FO CAG EiDIS 6 ONO. 0 CIBER CeO Cab Ione 3

f. Seam of light-grey sand and gravel .............-. 3 0
g. Ochreous gravel with an irregular seam of grey sandy
clay, containing Cyclas and Lamneus........02086

The two implements are supposed to have come from the bed g. aae

The seams are veryvariable. The gravel is subangular, and is com-
posed of fragments of flint, local Oolitic débris, pebbles of quartz and
of siliceous sandstones of the New Red Sandstone conglomerates, with
fragments of variousold rocks. In the lower bed are a considerable
number of small blocks of sandstone, oolites, and large flints. The
shells are dispersed throughout from a depth of 5 feet to the base.
They are mostly in fragments, but occasionally perfect. Ihave, with
the assistance of Mr. Pickering, determined the following species :—

Cyclas corneus. Bithinia tentaculata.

Pisidium amnicum. Limneus auricularis.
pulchellum. pereger.

Helix hispida. Planorbis carinatus.
pulchella. Valvata piscinalis.

A considerable number of the teeth and bones of the Elephas primu-
genius, Rhinoceros tichorhinus, and of the Horse, Ox, and Deer have
been found in this pit, chiefly at or near the bottom of the gravel. Now
it is evident that a certain portion of the materials of the gravel are
local, but still there is a large foreign element independently of the
flints. As thevalley drains only an oolitic district, which could not have
furnished any such materials, it is evident theymust have been derived
from the boulder clay, which caps the hills of the district and contains
all the required elements. The hills north of Bedford consist of boulder-
clay, b, as do also those west of Biddenham ; they both rise to a height
of about 100 feet above the river, and are separated by a valley
two miles broad. In this valley the gravel forms a wide, nearly level
tract, 60 to 80 feet lower than the hills, but still 20 to 40 feet above
the level of the present river. We have here therefore, as at
Hoxne, another good case of the flint-implement-bearing beds being
newer than the boulder-clay ; whilst in general physieal characters
and in the nature and variety of the organic remains we are strongly
reminded of the gravel beds of St. Acheul, near Amiens.

Surrey.—Twenty-five years ago, Mr. Whitburn, of Guildford, was
examining the gravel-pits at Peasemarsh, between that town and
Godalming, for fossil bones (of which a considerable number, inclu-
ding those of the Elephant, had been found here), when his attention
was attracted by a peculiarly shaped flint lying in a bed of sand,

VOL. XVII,—PART 1. 2¢

368 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

interstratified with the gravel, at a depth of about 4 feet from the
surface. He took it away and preserved it in his collection as an
object of antiquarian rather than of geological interest. Hearing,
however, of the late discoveries at Amiens and Hoxne, he sent the |
specimen, with an account of his finding it, to Mr. Evans. It is an
undoubted flint implement, rude and of a peculiar wedge-shaped
form. Ihave one specimen from St. Acheul with which it closely
agrees. This of course can be considered but as a possible instance.

Hertfordshire.—It is only ten days since Mr. Evans, while walk- ©
ing with some antiquarian friends from Nash Mills to Abbots
Langley, was struck with the great number of quartz, siliceous sand-
stone, slate, and other old rock-pebbles and fragments scattered over
a field near the latter place, and was still more surprised at finding,
among this surface-drift, a weathered flint implement with the top
broken off, but otherwise identical in form with the spear-head-
shaped specimens from Amiens and Herne Bay. Although found on
the surface, Mr. Evans, who is most competent authority on this point,
does not consider it to belong to the Stone-period. On the contrary,
he would refer it to the Pleistocene age. I have been with him to the
spot where it was found. The chalk hills are here about 200 feet above
the level of the Boxmoor valley, and are in places bare, and in other
places thinly covered with gravelly drift. Between this peculiar drift
and the flint implement I myself saw no connexion, and I can merely
mention the fact without venturing to speculate upon it.

We have thus, at all events, three additional counties in which Post-
pliocene flint implements have been found; and I would now direct
attention to a few other localities where there are beds of fresh-
water gravel and sand, or of freshwater and other associated gravels,
in which I think it highly probable that flint implements may occur.

Places for further Search.—I would more especially direct attention
to the gravel- and clay-pits at Copford, Lexden near Colchester,. and
Sudbury; the brick-pits at Erith, Grays, Ilford, Maidstone, and Salis-
bury; the low-level gravel-beds at or near Alton, Axminster, Bath,
Blandford, Brentford, Cambridge, Chartham, Chesterford, Chichester,
Chippenham, Croydon, Defford, Dover, Farnham, Faversham, Folk-
stone, Gloucester, Godalming, Hackney, Hertford, Hurley, Kingsland,
Oxford, Peasemarsh, Reading, Selsea, Stafford, Stamford, Stroud,
Taplow, Wandsworth, Westbury, Worcester, and Orton near Peter-
borough, as some of the places in the south of England where, I think,
flint implements may also, by diligent search, possibly be found. I say
<< diligent,” because even in places where they are most abundant,
as at St. Acheul, the search must be long before the observer is
rewarded by finding a single specimen; whilst in other places the
search often seems for a time almost hopeless. Judging from pre-
cedents, our motto should be Nil desperandum.

369

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From January 1st to March 31st, 1861.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

Albany. Twelfth Annual Report of the Regents of the University
of the State of New York. 1859.

American Journal of Science and Arts. Second Series. Vol. xxxi.
No. 91. January1861. From Prof. Silliman, For.M.G.S.

W. E. Logan.—Track of an Animal in the Potsdam Formation, 17
figures),

W Gibbs.—Platinum metals, 63.

J. L. Smith.—Guernsey County (Ohio) Meteorites, 87.

Bunsen.—New Alkaline metal, and Spectrum-analysis, 105.

C. List.—Copper in pig-iron, 115.

Th. Wichmann.—Preparation of Oxide of Lead free from Copper and
Tron, 117.

C. Tissier.—Action of Carbonate of Soda on Cast-iron, 120,

Geological Survey of Canada, Reports of, noticed, 122.

F. B. Meek and F. V. Hayden’s ‘ Fossils of Nebraska,’ noticed, 126.

B. F. Shumard’s ‘ Cretaceous Strata of Texas,’ noticed, 127.

F. Roemer’s ‘ Silurische Fauna des Texas,’ noticed, 127.

C. W. Eliot and F. H. Storer’s ‘On the Impurities of Commercial
Zinc,’ noticed, 142.

ee ‘Practical Treatise on Coal, Petroleum,’ &c., noticed,

Earthquake of Oct. 17, 1860, 150.

D. D. Owen, Obituary notice of, 153.

Army and Navy Club, Rules and Regulations, and List of Members,
1861.

Assurance Magazine. No. 42. January 1861.
2c2

370 DONATIONS.

Atheneum Journal. Nos. 1732-1744. January—March 1861.

Notices of Scientific Meetings, &c.

M. F. Maury’s ‘ Physical Geography of the Sea,’ noticed, 14.

R. Owen.—Land-saurians (Scelidosaurus and Phyllodosaurus) of the
Lias, 20.

J. Bewick’s “Geological Treatise on the District of Cleveland, in
North Yorkshire,’ noticed, 22.

Survey of the North Atlantic, 156.

R. Owen’s ‘ Essays, &c., by John Hunter,’ noticed, 317.

Cambridge (U.S.). Memoirs of the American Academy of Arts and
Sciences. New Series. Vol. vii. 1860.

Canadian Journal. New Series. No. 31. January 1861.
E. J. Chapman.—Stelliform Crystals, and the Crystallization of Snow,
1

W. E. Logan.—Fauna of the Quebec group of Rocks, and the “ Pri-
mordial Zone ” of Canada, 40.

M. Faraday.—Regelation, 54.

K. W. Brayley.—Apparent Universality of a principle analogous to
Regelation, 63.

EH. J. Chapman.—Tables for calculating the thickness of inclined
strata, 72.

Chemical Society. Quarterly Journal. No. 52.
Bolley.—Crystalline form of Metallic Chromium, 353.

Chemist and Druggist. Vol. 1. Nos. 17-19. January 15, 1861.

Bunsen and Kirchhoff’s Spectrum-analysis, 45.
H. M. Noad.—Analysis of Iron-ores, 77.

Critic. Vol. xxii. Nos. 548-560.
Notices of Scientific Meetings, &c.
EK. Hull’s ‘ Coal-fields of Great Britain,’ noticed, 148.
R. Damon’s ‘ Handbook to the Geology of Weymouth,’ noticed, 149.
H. Freke’s ‘On the origin of Species, &c.,’ noticed, 181.

Edinburgh Royal Society. Proceedings. Vol. iv. No. 50. 1860.

L. Playfair.—Numerical Relations between the Specific Grayities of
the Diamond, Graphite, and Charcoal forms of Carbon, and its
Atomic Weight, 241.

A. Murray.—Darwin’s ‘ Theory of the Origin of Species,’ 274.

T. Brown.—Lower Carboniferous Rocks of the Fiteshire Coast, 298.

A. Geikie.—Chronology of the Trap-rocks of Scotland, 309.

G. Robertson.—Solidification of Limes and Cements, 314.

T. Bloxam.—Composition of the Glassy Surface of some Vitrified
Forts, 338.

——, Transactions. Vol. xxi. Part 2. 1860.
T. Brown.—Mountain-limestone and Lower Carboniferous Rocks of
the Fifeshire Coast, 385. ;

——_—. Appendix to the Makerstoun Magnetical and Meteorological
Observations ; reduced and edited by B. Stewart, M.A. Supple-
ment to Vol. xxii. of the Transactions. 1860.

‘DONATIONS. 371

Geneva. Mémoires de la Société Physique et d’Hist. Nat. de Genéve.
Vol. xv. Deux. partie. 1860.

Plantamour.—Mesures hypsométriques dans les Alpes, 395.
E. Ritter.—Sur la figure de la Terre, 441.

Geologist. Vol. iv. Nos.37, 38. January and February 1861.

G. E. Roberts.—High and low Life, 1.

J. W. Salter.—Coal, 6, 59.

A. Delesse.—Pseudomorphs, 14.

S. J. Mackie.—F lint implements, 19.

T. Davidson.—British Carboniferous Brachiopoda, 41, 76.
J. Prestwich.—Section of Mundesley Cliff, 68.
Proceedings of Societies, 31, 71.

Notes and Queries, 36, 72.

Reviews, 40, 78.

Geologists’ Association. Proceedings. No.6. 1861.

ie Mitchell.—Application of Crystallography to Mineralogy and

reology, 65.

J. H. Mitchener._New Red Sandstone Quarry at Stourton in Che-
shire, 75.

J. Pickering.—Pleistocene Deposits, 78.

R. Bingham.—Geology of the Island of Sheppey, 92.

C. Rickman.—Strata and fossils at Peckham and Dulwich, 106.

India. Memoirs of the Geological Survey of India. Vol. ii. 1860.

H. B. Medlicott.—The Vindhyan Rocks, and their associates in Bun-
delcund, 1 (map).

J. G. Medlicott.—The Geological Structure of the Central Portion of
the Nerbudda District, 97 (2 maps).

W. Theobald.—The Tertiary and Alluvial Deposits of the Central
Portion of the Nerbudda Valley, 279 (map).

T. Oldham.—The Geological Relations and probable Geological Age
of the several systems of Rocks in Central India and Bengal, 299.

Lausanne. Bulletin de la Soc. Vaudoise des Sciences Nat. Vol. vi.
Bulletin No. 47. October 1860.

Michel.—L’hypsométrie du Bassin du Léman, 372.

C. Gaudin et G. de Rumine.—Coupe de l’axe anticlinal au-dessous
de Lausanne, 418.

Ch. T. Gaudin.—Nouveau Gisement de Feuilles fossiles 4 Lavaux, 456,

—. Flore des Travertins Toscans, 459.

——. Procédé pour calquer des Empreintes de Feuilles fossiles, 471.

Ph. Delaharpe.—Corne de renne du diluvium, 460.

EK. Collomb.—Silex ouvrés du dépét quartaire des bassins de la Somme
et de la Seine, 463.

R. Blanchet.—Goniobates Agassiz, 472 (plate).

H. Bischoffi—Sur Vacide hypermanganique, 473.

C. de Saporta.—Sur les plantes fossiles de la Provence, 505.

Linnean Society. Proceedings. Supplement to Vol. vii—Botany.
Dec. 31, 1860.

372 DONATIONS.

Literary Gazette. New Series. Vol. vi. Nos. 132-142, 144.
Notices of Scientific Meetings, &c.
E. Hull’s ‘ The Coal-fields of Great Britain,’ noticed, 19.
C. S. Forbes’s ‘Iceland, its Volcanos, Geysers, and Glaciers,’ noticed,

35.
Wogel.—Old Lobenic paalstabs, 230.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxi. Nos. 137-139. January-March 1861. From Dr. W.
Francis, F.G.S.

F, W. and A. Dupré.—The existence of a fourth Member of the Cal-
cium Group of Metals, 86.

D. Forbes.—Geology of Southern Peru and Bolivia, 154.

T. H. Huxley.—Macrauchenia Boliviensis, 156.

J. W. Salter.—Paleozoic Fossils from Bolivia, 156.

T. A Hirst.—Ripples, and their relation to the Velocities of Currents,

88.

J. Nicol.—Structure of the N.W. Highlands, 235.

T. F. Jamieson.—Structure of the S.W. Highlands, 235.

H. Mitchell —Old Red Sandstone of Forfarshire, 256.

P. B. Brodie.—Corals of the Lias, 237.

W. S. Symonds.—Malvyern and Ledbury Tunnels, 2387,

F, W. and A. Dupré.—Calcium Spectrum, 239.

London Review. Vol. ii. Nos. 33-39. February and March 1861.
Notices of Scientific Meetings, &c.
E. Hull’s ‘Coal-fields of Great Britain,’ noticed, 187.
Loss of Life in Collieries, 199.
M. Faraday.—Platinum, 231.
Stones of the Palace of Westminster, 282.

Longman and Co.’s Notes on Books. Vol. ii. No. 24. Feb. 28,1861.

Mechanics’ Magazine. NewSeries. Vol. v. Nos. 107, 108, 110-116,
118.
Notices of Scientific Meetings, &c.
J. W. Tayler.—Greenland and its Ice, 25 (figures).
Decay of Building-stones, 85.
Profiles of the North Atlantic, 105 (figures).

Montreal. Canadian Naturalist and Geologist. Vol. v. No. 6.
Dee. 1860.
E. Billings.—On certain Theories of the Formation of Mountains,
409.
F. Bradley and E. Billings.—New Trilobite (Conocephalus minutus)
from the Potsdam Sandstone, 420 (figures).
J. W. Dawson’s ‘ Acadian Geology’ and ‘Supplement,’ noticed, 450.
J. W. Dawson.—Cyclopteris Acadica, 460.
W. E. Logan.—Quebec Group of Rocks and the Primordial Zone of
Canada, 472.
Neuchatel, Bulletin de la Société des Sciences Nat. de. Vol. v.
Part 2. 1860.
Mortillet.—Sur la structure et la formation des lacs, 185.

Desor.—Sur les instruments fossiles d’Amiens, 206,
Kopp.—Tremblements de Terre 4 Neuchatel dans le 17mesiécle, 279.

—

DONATIONS. 3703

Neweastle-upon-Tyne. Transactions of the Tyneside Naturalists’
Field-club. Vol. iv. Part 4. 1860.

J. W. Kirkby.—Permian Chitonidee, 238 (plate).

New Zealand Examiner. Nos. 12-15. December 17, 1860—March
19), ILS Kou be

Taranaki Steel, 218, 245,

Palzontographical Society. Monographs. 1861.

Wright, T.—A Monograph on the British Fossil Echinodermata from
the Oolitic Formations. Part iv. pages 391-469, plates 37-43.
Edwards, F. E.—A Monograph of the Eocene Mollusca. Part iii.

No. 5. Prosobranchiata, continued.

Owen, R.—Monoeraph of the Fossil Reptilia of the Cretaceous and
Purbeck Strata,—including Supplement No. 3 to the Monograph on
the Fossil Reptiliaof the Cretaceous Formations—Cretaceous Ptero-
sauria and Sauropterygia; Supplement No. 2 to the Monograph
on the Iguanodon; and a Monograph on the Fossil Lacertian
Reptiles of the Purbeck Limestones.

Davidson, T.—A Monograph of British Carboniferous Brachiopoda.
Part v. No. 3.

Paris. Annales des Mines. 5° Sér. Vol. xvii. 2° Livr. de 1860.

Ch. Heusser et G. Claraz.—Gisement et exploitation du diamant dans
la province Minas Geraes au Brésil, 289.

Vol. xvi. 98° Livr. de 1860.

Hstaunié.—Des diverses variétés de houille du département de Sadne-
et-Loire, 367.

Gonot.—Sur lindustrie minérale de la province de Hainaut (Bel-
gique), 493.

G. Boilleau.—Sur les mines de cuivre découvertes prés d’Acton, pro-
vince de Montréal (Canada), 510.

Bibliographie (prem. semestre de 1860), 523.

Vol. xvii. 4° Livr. de 1860.

S. Gras.—Sur Vopposition que l’on observe souvent dans les Alpes
entre lordre stratigraphique des couches et leurs caractéres paléon-
tologiques, suivi d’un nouvel exemple de cette opposition, 17.

Morin et Tresca.—Détermination du coefficient d’élasticité de l’alu-
minium, 63.

H. Sainte-Claire Deville et H. Debray.—De la métallurgie du platine
et des métaux qui l’accompagnent, 71.

A. Delesse.—Recherches d’azote et des matiéres organiques dans
V’écorce terrestre, 151.

a

Mémoires de l’Acad. des Sciences de l'Institut Impérial de
France. Vol. xxviii.

——. Comptes Rendus hebdom. des Séances de l’Acad. des Sciences,
1860, Deux. Semestre. Vol. li. Nos. 23-26.

—. ——. 1861, Prem. Sem. Vol. lu. Nos. 1-5.

374 DONATIONS.

Paris. Soc. Géol. de France. Bulletin de, pp. 1025-1158. Reé-

union extraordinaire 4 Lyon (Rhone) du 1% au 11 Septembre,
1859.

Gras, S., et Fournet.—Sur les caractéres du terrain de transport connu
aux environs de Lyon sous le nom de “diluvyium alpin” ou de
“ conglomérat bressan,” 1028, 1033.

Fournet.—Sur les phénoménes du lehm, 1049.

Sur le mont d’Or et sur son systéme triassique, 1088.

—. Sur les cailloux impressionnés, 1103.

. Sur les roches schisteuses dites ‘ cornes vertes” et “cornes |
rouges,” 1151.

Th. Ebray.—Sur la constitution géologique du dép. du Mont-d’Or,
1059.

EK. Dumortier.—Sur le terrain jurassique du Mont-d’Or, Lyonnais,
1065.

——. Sur les tufs calcaires de Meximieux, 1099.

Fisserandot.—Sur le terrain houiller de Ternay et de Communay,
1115.

Drian.—Sur le terrain houiller de Communay, 1116.

Bulletin de la Société Géologique de France. Deux. Sér.
Vol. xvii. Few. 45-52. 1860.
Melleville-—Description géologique de la montagne de Laon, 710.
J. Cornuel.—Sur le groupe de grés vert inférieur du bassin de la
Seine, etc., 736.
Bureau.—Sur l’existence de trois étages distincts dans le terrain dé-
vonien de la Basse-Loire, 789.
Ch. Lory.—Sur le gisement de la craie blanche dans la vallée d’En-
tremont (Savoie), 789.
Hébert.—Sur le travertin de Champigny et sur les couches entre les-
quelles il est compris, 800.
Em. Goubert.—Schistes & Lucines dans le gypse d’Argenteuil, 812.

Philadelphia Academy of Nat. Sciences. Proceedings. Sheets 19-42.

F. B. Meek.—New Species of Fossils from Nebraska, 28.

W. M. Gabb.—Belosepia Ungula from Texas, 324.

F. B. Meek and A. H. Worthen.—New species of Carboniferous Cri-
noidea and Echinoidea, 379.

F. B. Meek and F. V. Hayden.—Catalogue of Jurassic, Cretaceous,
and Tertiary Fossils from Nebraska, 417.

ff. C. Wood.—Carboniferous Flora of the United States, 436, 519.

F. B. Meek and A. H. Worthen.—New Species of Carboniferous Fos-
sils from Iowa, Ilinois, &c., 447.

J. Marcou.—Jurassic Fossils of New Mexico, 548.

W. M. Gabb.—New Species of Tertiary Fossils from Central Ame-

rica, 567,

Journal. New Series. Vol. iv. Part 4. 1860.

W. M. Gable.—Descriptions of New Species of American Tertiary
and Cretaceous Fossils, 875 (3 plates).

——. American Philosophical Society. Laws and Regulations, and
List of Members, 1860.

Proceedings.
Emerson.—Phosphorescence of Diamond, 175.

DONATIONS, 375

Philadelphia. American Philosophical Society. Transactions. New
Series. Vol. xi. Part 3. 1860.

Photographic Society. Journal. Nos. 105—107.

Quarterly Journal of Microscopical Science. New Series. No. 1.
January 1861.

Ray Society. A History of the Spiders of Great Britain and Ire-
land. By John Blackwall. 1861.

Royal College of Physicians. List of Fellows, &c. 1860.

Royal Dublin Society. Nos.18 and19(inone). July and October
1860.
S. Haughton.—Axctic Fossils, 53 (4 plates).
W. J. Wonfor.—Analyses of the White Limestone of Antrim, 77.

J. Birney.—Solubility of Granite in solutions of the Ammoniacal

Salts, 80.
Royal Geographical Society. Journal. Vol. xiii. 1860.

Address and Obituary Notices, c.

C. Levin.—Mexico [ Mines, &c.], 1 (Map).

H. de Saussure.—Ancient Volcano (San Andres) in Mexico, 53.

E. G. Squier.—Lake of Yojoa in Honduras, 58 (Map).

G. J. Pritchett.—Kcuador, 64 (Map).

L. Oliphant.—The Yangtze or Ta-Kiang, 75 (Map).

J. Stokes.—The Lower Danube, 162 (Map).

J. Sanderson.—Orange River Free State, &c., 233 (Map).

E. Palmer.—St. Helena, 260.

J. Palliser and J. Hector—Country between Lake Superior and
Vancouver Island, 267 (Map).

Royal Horticultural Society. Proceedings. Vol. vi. Nos. 20, 22.
January and March 1861.

Royal Society. Proceedings. Vol. xi. No. 42.
W. J. Bowditch.—Coal-gas, 25.

Society of Arts. Journal. Nos. 424-436. January-March 1861.
Consular Information, 98, 110, 197, 224.
G. R. Burnell. Water-supply of London, 169.
H. Wilkins.—Rock-oil, 179.
A. K. Isbister—Hudson Bay Territories, 230.
H. W. Revelly.—Ventilation of Mines, 262.
D. T. Ansted.—Arrangement of Minerals and Mineral Manufactures
at the Exhibition of 1862, 277.
C. Tomlinson.—Paraffine, 295.

Victoria, Philosophical Institute of. Transactions. Vol. iv. Part 2.
1860.

J. E. Woods.—Some Tertiary Rocks at Portland Bay, 169.

W. L. Morton.—Northern District of Queensland, 188 (Map).

P. Nissen.—Hlementary Substances originating and promoting Civi-
lization, xxxv.

J. Macadam.—Spurious Gold in Victoria, li.

——. Guano-deposit in Port Phillip Bay, li.

Black Auriferous Sand from the Nicholson Diggings, liii.

Report on the Resources of the Colony of Victoria.

37 6 DONATIONS.

Vienna. Sitzungsberichte d. K. Akad. d. Wissensch., Math.-naturw.
Classe. Vol. xxxix. No.6. 1860.

K. von Hauer.—Ueber eine selensaure Salze, 837.

P. Weselsky.—Analysen einiger Mineralien und. Hiittenproducte,
841.

A. Weiss und A. Schraaf.—Revision der vorhandenen Beobachtungen
an krystallisirten Korpern, mit einem Vorworte von Prof. A.
Schrotter, 853.

Wolly adi, INoke 10), USO,

F, Rolle.-—Die Lignit-Ablagerung des Beckens von Schénstein in
Unter-Steiermark, 7 (1 map and 2 plates).

Fr. Unger.—Die Pflanzenreste der Lignit-Ablagerung yon Schén-
stein, 47 (2 plates).

G. Tschermak, —Analyse des Datolithes von Toggiana, 60.

Fr. von Hauer.—Cephalopoden-Fauna der Hallstatter Schichten, 113
(5 plates).

W. Haidinger.—Der Meteorit von Shalka in Bancoorah und der Pid-
dingtonit, 251.

G. Bizio—Analisi chemica dell’ acqua minerale, detta Salsa o di 8.
Gottardo, in Ceneda, Provincia di Treviso, 335.

F, von Zepharovich.—Ueber die Kry stallformen des essig o-salpeter-
sauren Strontian und des weinsteinsauren Kali- Lithion, 516 (2
plates).

xeuman Lang.—Ueber das Gesetz der rationalen Verhiltnisse der
Tang enten tautozonaler Krystallkanten, 525.

R. Niemtschik.—Ueber die directe Construction der schiefaxigen
Krystallgestalten aus den Kantenwinkeln, 535 (1 plate).

Fy. Wohler.—Ueber die Bestandtheile des Meteorsteines vom Cap-

land, 565.

ie Haidinger.—Einige neuere Nachrichten tiber Meteoriten, 568,
745.

A. Schrétter—Ueber das Vorkommem des Ozons im Mineralreiche,
TOR
(20.

A. Schrauf.—Bestimmung der optischen Constanten krystallisirter
Korper, 769 (2 plates).

A. Schrotter.—Ueber eimige Producte aus der Saline zu Halstatt,
QO5.

——. Vol. xli. No. 21. 1860.

W. Haidinger.—Der Meteorit von St.-Denis-Westrem, 9.

H. Dauber. —Ermittelung kvystallographischer Constanten und des
Grades ihrer Zuverlas sigkeit, 19 (12 plates).

A. E. Reuss.—Die fossilen Molluske der tertiiren Stisswasserkalle
Bohmens, 55 (8 plates).

Washington. Smithsonian Contributions to Knowledge. Vol. xi.
1860.

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. vi.
Nos. 37-39. January-March 1861.

DONATIONS. 377

Edinburgh New Philosophical Journal. New Series. Vol. xiii.
No.1. January 1861.

W. L. Lindsay.—The Eruption, in May 1860, of the Kotlugja Vol-
cano, Iceland, 6 (map).

R. Edmonds.—The Earthquake-shock in Cornwall on the 13th of
January 1860, 100.

W. Thomson.—New Paleozoic Group of Echinodermata, 106

lates).

ofR. neue ‘Species not transmutable,’ noticed, 128. :

J. Bewick’s ‘Geological Treatise on the District of Cleveland in
North Yorkshire,’ noticed, 133.

— Stur.—Coal-plants of Bohemia, 158.

J. Nicol.—Geology of the N.W. Highlands, 159.

— Hayes.—Ivon of Liberia, Africa, 165.

Acton Copper-mine, 166.

W. P. Blake.—Stephanite, brittle silver-ore, from Washoe, 167.

W. B. Rogers.—The Albert Coal of New Brunswick, 167.

Institut, ’. I Section. Nos. 1407-1419; and II* Section. Nos.
296-298.

Notices of Meetings of Scientific Societies, &c.

Leonhard und Bronn’s Neues Jahrbuch fiir Min., Geol. u.s.w. Jahrg.
1860. Sechtes und Siebentes. Hefte.
J. Barrande.—Ueber die regelmassige periodische Abstossung der
Schaale bei gewissen palaolithischen Cephalopoden, 641 eae
Dondorff:—Beitrag zur Kenntniss der Puddelschlacke, 668 (plate
Zeuschner.—Die Brachiopoden des Stramberger Kalkes, 678.
J. Barrande.—Neue Beweise einer western Verbreitung der Primor-
dial-Fauna in Nord-Amerika, 769.
D. Fr. Wiser.—Krystallographische Mittheilungen, 784.
Letters: Notices of Books, Mineralogy, Geology, and Fossils.

——. Jahrg. 1861. Erstes Heft.

O. Volger.—Adular-Felspath als Mortel und Gangart in Schiittigen
Fels-Massen des Sachsischen Kohlen-Gebirges, 1.

Fr. Scharff—Ueber die Bildungsweise des Aragonits, 32 (plate).

O. Heer.—Ueber die fossilen Calosoma-Arten, 52.

Letters: Notices of Books, Minerals, Geology, and Fossils.

[Index for the years 1850-59.| Allgemeines Repertorium
der Min., &. 1861.

Paleontographica. (H. von Meyer.) Vol. vii. Part 4. Dec. 1860.
H. von Meyer.—Die Prosoponiden oder Familie der Maskenkrebse,
183 (pl. 23).

Acteosaurus Tommasini aus dem schwarzen Kreide-Schiefer
von Comen am Karste, 223 (pl. 24).
Coluber (Tropidonotus ?) atavus aus der Braunkohle des Sie-
bengebirges, 232 (pl. 25).
. Saurier aus der Tuff-Kreide von Maestricht und Folx-les-
Caves, 241 (pl. 26).

. Lamprosaurus Goepperti aus dem Muschelkalke von Krappitz
in Oberschlesien, 245 (pl. 27, fig. 1).
Phanerosaurus Naumanni aus dem Sandstein des Rothliegen-
den in Deutschland, 248 (pl. 27, fig. 2-5).

378 DONATIONS.

Paleontographica. (H.von Meyer.) Vol. vii. Part 6. Jan. 1861.

G. Fresenius.—Ueber Phelonites lignitum, Ph. strobilina, und Betula
Salzhausenensis, 155 (plate).

R. Ludwig.—Fossile Pflanzen aus dem tertiaéren Spatheisenstein von
Montabauer, 160 (8 plates).

. Stisswasser-Bewohner aus der Westphalischen Steinkohlen-
Formation, 182 (2 plates).

——. Stisswasser-Bivalven aus der Wetterauer Tertiar-Formation,
195 (plate).

Ili. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors im Italics.

Barrande, J. On the Primordial Fauna and the Taconic System ;
with additional Notes by Jules Marcou. 1860. From M. Jules
Marcou.

Berchem, J. P. Br. Itinéraire de la Vallée de Chamonix, d’une partie
du Bas Vallais et des montagnes avoisinantes. 1790. rom L.
Horner, Esq., Pres.G.S.

Botfield, B. Shropshire, its History and Antiquities. 1860.

?Bourrit. Voyage pittoresque aux glaciers de Savoye, fait en 1772.
1773. From L. Horner, Esq., Pres.GS.

Bronn, H. G. Essai d’une Réponse a la question de prix proposée
en 1850 par l’Acad. des Sciences, &c. 1861.

——. Catalogue annuel de la Librairie Francaise. Vol. ui. Année
1860. 1861. From Messrs. Dulau and Co.

Catalogue. Verzeichniss der Bibliothek des Professors Dr. C. Ritter
in Berlin. 1861. From the Publishers.

Clarke, W. B. Researches in the Southern Gold-fields of New South
Wales. 1860.

Collini. Journal d’un voyage qui contient différentes observations
minéralogiques particuliérement sur les Agates et Basalte. 1776.
From L. Horner, Esq., Pres.G.S.

Deslongchamps, E. Note sur le genre Hucyclus, nouvelle coupe
établie pour quelques coquilles des terrains Jurassiques. 1860.

Observations concernant quelques Gastéropodes Fossiles des
Terrains Jurassiques, placés par l’auteur de la Paléontologie Fran-
eaise dans les genres Purpurina, Trochus, et Turbo. 1860.

Evans, J. Flint Implements in the Drift. 1860.

Faure, A. Note sur le Terrain Houiller et sur le Terrain Nummu-
litique de la Maurienne. 1861.

. a

DONATIONS, 793

Ferrel, W. The Motions of Fluids and Solids relative to the Earth’s
Surface, comprising applications to the Winds and Currents of the
Ocean. 1860.

Forbes, J. D. Reply to Prof. Tyndall’s Remarks, in his work “ On
the Glaciers of the Alps,” relating to Rendu’s “Théorie des Gla-
ciers.” 1860.

Fougt, H. Dissertatio Corallia Baltica adumbrans. 1745. From
L. Horner, Esq., Pres.GS.

Freke, H. On the Origin of Species by means of organic affinity.
1861.

Gibb, G. D. On Canadian Caverns. 1861.

Gray, A. Natural Selection not inconsistent with Natural Theology.
1861.

Hall, J. Report on Canadian Graptolites. 1858.

Hauer, F.,v. Nachtriige zur Kenntniss der Cephalopoden-Fauna der
Hallstitter Schichten. 1860.

Hébert, EZ. ect E. E. Deslongchamps. Mémoire sur les fossiles de
Montreuil-Bellay (Maine-et-Loire). 1860.

Helmersen, G. v. Das Olonezer Bergrevier. 1860.

Hill, J. A General Natural History ; a new and accurate Description
of the Animals, Vegetables, and Minerals of the different parts
of the World. 1743. From Mr. Charlton.

. An History of Animals, containing Descriptions of the Birds,
Beasts, Fishes, and Insects of the several Parts of the World.
1752. From Mr. Charlton.

Hull, H. On the Vestiges of Extinct Glaciers in the Highlands of
Great Britain and Ireland. 1861.

The Coal-fields of Great Britain, their history, structure, and
duration; with notices of the Coal-fields of other Parts of the
World. 1861.

Jamieson, T. F. List of Altitudes in the Counties of Aberdeen,
Banff, and Kincardine.

——. The Tweeddale Prize Essay on the Rainfall. 1860.
Lea, I. Observations on the Genus Unio. Vol. viii. part 1. 1860.

Lindsay, W. L. On the Eruption in May, 1860, of the Kotlugja
Volcano, Iceland. 1861.

Lubbock, J. Leydig’s Natural History of the Daphnide. 1861.

—. Onsome Occanic Entomostraca collected by Captain Toynbee.
1861.

380 DONATIONS.

Lubbock, J. On Spherularia Bombi. 1861.

M: Andrew, FR. List of the British Marine Invertebrate Fauna.
1860.

Magnetical and Meteorological Observations made at the Government
Observatory, Bombay, in the year 1858. 1859. From the Indian

Government.

Naumann, C. T, Lehrbuch der Geognosie. Zweiter Band. Erste
Abtheilung. 1860.

Nicol, J. On the Structure of the North-western Highlands, and
the Relations of the Gneiss, Red Sandstone, and Quartzite of
Sutherland and Ross-shire. 1861.

Oldham, T. On some fossil Fish-teeth of the genus Ceratodus, from
Maledi, South of Nagpur. 1861.

On the Geological Relations and probable Geological Age of
Rocks in Central India and Bengal. 1861.

Owen, R. Memoir on the Megatherium or Giant Ground-sloth of
America (Megatherium Americanum, Cuvier). 1860.

Patrin, E. M.S. Histoire Naturelle des Minéraux. 1803. From
L. Horner, Esq., Pres.GS.

Pole, W. Diamonds. 1861. From Prof. J. Tennant, F.G.S.

Report of the Superintendent of the Coast-survey, showing the Pro-
gress of the Survey during the year 1858. 1859.

Reports of Explorations and Surveys to ascertain the most practica-
ble and economical route for a railroad from the Mississippi River
to the Pacific Ocean. 1853-1856. Vol. xi. 1855.

Ruschenberger, W. 8. W. A Notice of the Origin, Progress, and
present Condition of the Academy of Natural Sciences at Philadel-
phia. 2nd edition. 1860. From the Acad. Nat. Sc. Philadelphia.

Sandberger, F. Die Conchylien des Mainzer Tertiiirbeckens. Vierte
Lieferung.

Scharff, F. Ueber die Bildungsweise des Aragonits. 1861,

Suess, E. Eimige Bemerkungen iiber die secundiren Brachiopoden
Portugals. 1860.

Ueber die Spuren eigenthtimlicher Eruptions-Erscheinungen
am Dachstein-Gebirge. 1860.

Thomson, W. On anew Paleozoic Group of Echinodermata. 1861.

Tylor, E. B. Anabuac: or Mexico and the Mexicans, ancient and
modern. 1861.

THE

QUARTERLY JOURNAL

OF

THE GEOLOGICAL SOCIETY OF LONDON.

PROCEEDINGS

OF

THE GEOLOGICAL SOCIETY.

Aprit 10, 1861.

James Hector, M.D. Edinb., 13 Gate Street, Lincoln’s Inn Fields,
was elected a Fellow.

The following communications were read :—

1. On Exxvations and Depressions of the Kartu in NortH AMERICA.
By Asranam Gusner, M.D., F.G.S.
: (Abridged. )

United States.—Commencing at New Jersey, in the United States,
the writer has examined nearly all the most interesting parts of the
coasts, as far northward as the northern part of Labrador. The
whole south-eastern side of New Jersey, where it borders upon the
Atlantic, to the extent of 100 miles in length and about 20 miles in
breadth, is composed of alternate strata of sand, greensand, marl,
and clay, some of the beds very highly fossiliferous. The land is
comparatively low, and slopes gradually from the high lands in the
rear towards the sea. A similar tract of country occurs in the
bordering State of Maryland, and, still further southward, in North
Carolina.

VOL, XVII,—PaRT I. 2D

382 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

The oldest inhabitants of New Jersey, whose lives have been ex-
tended to upwards of eighty years, maintain that within a period of
sixty years the sea has risen upwards of four feet, or, what is equi-
valent thereto, the coast has fallen to that depth. Marshes that
were formerly mowed for their grass are now submerged; the sea has
encroached upon the land, even over the sites of ancient habitations.
There are tracts where trees are seen growing upon fallen forests,
which have been buried in sand and peat. ‘Timber of excellent de-
scription is dug out of the present marshes. The amount of depression
along this coast is variously estimated as being from 5 to 12 feet.

From these, and other facts which might be quoted, it appears
that there are marine Cretaceous deposits, and over them Pleistocene
deposits with freshwater shells and Mastodon bones, and apparently
an old forest buried in sand, with the remains of another growing
over it—these two being under the sea in some places and therefore
proving submergence of a land-surface,—and that this submergence
is still going on, according to the testimony of the inhabitants and
the submergence of habitations.

In the harbour of Nantucket, there is a submarine forest. In
dredging the estuary, Lieutenant Prescott found trunks and roots of
the cedar, oak, maple, and beech, some of them standing upright and
still attached to the soil on which they flourished. Excepting the
cedar, all the woods are still sound. The trees are partially buried
in sand, and are eight feet below the level of the lowest tide.

A similar submarine forest exists at Holme’s Hole, on Martha’s
Vineyard. On the west side of the harbour, stumps of trees are
found standing upon a level surface beneath the water; another
woody tract occurs near the south-west extremity of the Vineyard,
and on the north side of Cape Cod, opposite Yarmouth: the latter
extends more than three miles into Barnstable Bay. At Portlanda
similar sinking of the land has been clearly made out. In none of
these instances is there any accounting for the facts, but by actual
subsidence. No indications of elevation were observed in this
quarter.

New Brunswick.—Proceeding in a northerly direction, we arrive
at the River Schoodiac, or St. Croix, the dividing-line between the
United States and the British Province of New Brunswick. Instead
of submergence, an elevation of the land is here clear and distinct.
It extends in a northerly direction upwards of twenty miles, and
probably to a still greater distance along the coast in the direction
of the Bay of Fundy. The greatest elevation is near the centre of
this area, which has been but little raised at its edges. The solid
rocks beneath the modern marl-beds are chiefly red sandstone,
syenite, and granite, with intrusions of trap-rocks.,

At St. Andrew’s, St. Stephen’s, Lubec, Eastport, and numerous
sites in the adjacent districts, there are extensive deposits of sand,
marl, and marly clay, containing relics of shells and sea-weeds which
still inhabit the present shores ; and the former are so numerous, that
they have contributed sufficient lime to some of the strata to render
them valuable for fertilizing-purposes. At first these mazl-beds were

1861.] GESNER—MOVEMENTS OF LAND. 383

supposed to be Tertiary deposits; but late observations have deter-
mined their more recent origin. The greatest elevation observed
was near the town of St. Andrew’s, where the marl with recent shells
is found 28 feet above the level of the highest tide.

Among the numerous islands of Passamaquoddy Bay the writer
observed many of the indications of elevation ; nor is it difficult to
discover along the borders of the creeks and rivers the sites from
which the sea has been slowly and gradually withdrawn. Strata
of marl and clay with shells like those before mentioned appear
at Beaver Harbour, where the elevation has been less considerable.

Grand Manan is a beautiful island, situated off the mouth of the
St. Croix River, and 12 miles from the American line. It is 25 miles
long and 5 miles in breadth. The north-west side is a somewhat
lofty ridge of trap-rock, uninhabited and presenting to the sea per-
pendicular and overhanging cliffs. The opposite side of the island
is inhabited; and the industry is agriculture and fishing; and a number
of small islands and harbours afford shelter for vessels.

The most remarkable circumstance connected with this isolated
part of New Brunswick is the fact, that the entire south side of the
main and its islets have within a recent period been submerged to
the depth of 18 feet and upwards. There still remains a tradition
that there once existed between the main, the three Duck Islands,
and Nantucket Island a kind of marsh of several thousands of acres.
This marsh has slowly disappeared beneath the sea ; and its surface is
only partially uncovered by the water at the lowest spring-tides.
The roots, stumps, and trunks of a great number of trees (the pine,
hemlock, and cedar) stillremain firmly attached to the sunken earth,
and at the very sites where they flourished. The once living forest
with its branches and leaves is now deeply covered by each suc-
ceeding tide. The anchors of small craft are often held fast among
the wood of the bottom of the harbour. It was by this subsidence
that several islands became isolated ; for the marshes that formerly
attached them one to the other have been denuded and washed away
by the waves. The subsidence extended to the distance of several
miles westward; but it is best measured near the small islands
before mentioned. Viewed altogether, it would seem that Grand
Manan has slowly moved upon its axis, depressing one side and
elevating the other.

At the mouth of the River St. John and at the city of the same
name, in the Province of New Brunswick, the evidences of elevation
are distinct over an area of twenty square miles. Between the city
and Portland, there is a narrow and deep valley now occupied by a
church, manufactories, and dwelling-houses. In this valley, and
above strata of clay, there are marl-beds containing marine shells
and decomposed sea-weeds identical with those still inhabiting the
shores of the harbour. These beds are about 18 feet above the
level of the sea, which at some former period surrounded the site of
the city.

At Manawagonis, Mispec, Emerson’s Creek, and many other places

in this quarter, there are beds of sand, clay, marl, and marly clay
2 De2:

384 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

exposed to the sea, forming low and almost level tracts along its
borders. Similar deposits also occur in the banks of the St. John
and Kenebecacis Rivers, above the reach of the highest tides. They
not only appear where the currents have exposed the beds, but also
remote from those streams. The shells are chiefly imbedded in the
sand and marl, which also contain the relics of recent marine vege-
tation. In these deposits upwards of twenty genera of recent Tes-
tacea and six genera of Crustacea have been obtained. Some of the
shells, such as the Mya mercenaria, Pecten, Arca, &e., are well
preserved. The shells of the Solen ensis and Mytili are too brittle
to be removed. The claws of crabs and the bones of fishes, although
changed, are not destroyed. ‘The shells of the uppermost beds are
more decayed than those of the lower deposits, and appear as
though the elevation had been slow and gradual, and not sudden
like those frequently indicated in districts moved by earthquakes.
The strata containing these remains are now from 10 to 40 feet
above the level of the tides, which rise 30 feet along this part of the
coast at spring-tides.

The rivers emptying into the Bay of Fundy along this line of
coast are broken by falls at their mouths; but the streams which do
not pass through this raised district empty themselves into the bay
smoothly and withoutinterruption. It is therefore not unreasonable
to believe that the breaking-up of the river-beds was coeval with the
elevation of the shelly deposits now removed far above the reach of
the waves.

The next site to be noticed is remarkable for its submergence ; it
is called the Great Tantamar Mash, situated 120 miles eastward
of the St. John, in the County of Westmoreland, and at the head-water
of Chignecto Bay. This marsh is 13 miles long, and about 4 miles
broad. Large tracts have been rescued from the sea by embank-
ments, or “ dikes,’”’ thrown up on the borders of the river and its
creeks. Atthe eastern extremity of the Tantamar, there is a sunken
tract, composed of peat-bog, floating bogs, with swamps and small
lakes, not less than 8 miles long and 3 miles in width. It is the
breeding-place of great numbers of wild ducks and snipes. Large
trees of different kinds, collections of shells, bones of fishes, &e.
appear at different depths in the alluvium. But besides these, on
the northern border of the alluvial deposit, patches of forest-trees,
some of which have been felled by the woodman’s axe, are now over-
flowed by the tides. Relics of the early French settlers, Indian har-
poons, and pieces of their bark canoes, and other traces of the
aborigines have been dug up at depths of 5 and 10 feet beneath
the surface, on the opening of canals and ditches remote from the
river.

The same depressing influence has been at work at Shediac and
Bay Verte. At the latter place the gravestones of persons killed by
the Indians in 1755 are now reached by the tide at high water,
which washes the base of old Fort Moncton, and rises above its
causeway.

In the County of Northumberland, where it borders upon the Bay

1861.] GESNER—MOVEMENTS OF LAND. 385

de Chaleurs, there has been a depression, evidently slow in its progress
and continued. In the vicinity of Bay des Vents and Lower Bay des
Vents, extensive peat-bogs are seen at low water reaching outwards
beneath the sea: the peat is of super-marine growth, and its highest
parts are scarcely above the tide-level. The shores are low and
level ; and evidences of land-slides are absent. At Bathurst, on the
contrary, and on the opposite shore of Lower Canada, there has been
an elevation of several feet, and which apparently is still progressing.
A number of minor elevations and depressions were observed during
the writer’s geological survey of the Province, before leaving which
the terraces along the Upper St. John River may be adverted to, as
being connected with this subject.

On the banks of this river we frequently observe, in ascending
from its borders, several parallel steps which rise abruptly from one
level to another in succession. These steps are composed of diluvial
matter, in which there are occasionally contained decayed timber and
fragments of freshwater shells. These are well displayed near the
ferry four miles below Woodstock.

Section of the Terraces near Woodstock, New Brunswick.
Be

a. The river.

6. First terrace, 22 feet above the level of the river.
c. Second terrace, 28 feet above the level of the river.
d. Third terrace, 40 feet above the level of the river.

These several terraces mark distinctly the former banks of the
river, which has been withdrawn from its ancient limits to a narrow
channel with an increased velocity of current. Near the mouth of
Maduxnakeag, a tributary of the St. John, the ancient bed of the
stream is now dry and under cultivation. Whether these terraces
have been produced by an uplifting or depressing force, it is difficult
to ascertain. It is probable, however, that the site of the river was
oncealake, which has been drained.by the yielding of the earth further
down the stream, where there are now violent rapids and marks of
recent terrestrial disturbance. Terraced valleys are common on
many of the rivers of North America.

Nova Scotia.—At many places in Nova Scotia, changes of level on
the surface of the earth appear very distinct, although they are less
manifest than they are in the sister Province. It is generally main-
tained by aged persons, that the tides flowing into the Bay of Fundy
and Minas Basin and its numerous rivers and creeks are rising.
The records of ancient landmarks, the encroachment of the water
upon the dry earth, the discovery of ancient bridges and relics of the
native Indians beneath the present tide-level, corroborate ‘that
opinion. At numerous places in the marshes of the Shubenacadia,
Avon, and King’s County Rivers, the alluvia of the sea are perfectly

386. PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

stratified. Some of these strata and those called “blue marsh” are
composed in part of plants still undergoing decomposition and ex-
pelling carburetted hydrogen. These strata are sometimes 12 feet
beneath the surface, and interlaid with beds of alluvium, which, when
their layers are exposed, display with beautiful distinctness the tracks
of the numerous wading birds that frequent the shores. Itis almost
unnecessary to add that sea-alluvia never accumulate above the
highest tide-mark.

On the southern side of this Province, where it meets the Atlantic,
the old fishermen universally report the effects of uplifting at certain
places where they have been wont to anchor their nets and boats in
pursuing their avocation. Off the harbour of Halifax, and Sambro
Lighthouse, a submarine elevation appears to be advancing. <A few
years ago a steamer was wrecked in breakers six miles south of
the lighthouse, after a gale of wind: breakers at that place were
unknown before. Recent soundings also show a shallowing of the
water.

Cape Breton.—In the Island of Cape Breton, situated at the
entrance of the Gulf of St. Lawrence (and which the writer had an
opportunity to explore under the patronage of the late noble Earl of
Dundonald), several upheavings and depressions of the land were
observed, not dissimilar to those already mentioned. Among the
latter is that of the ancient city of Louisburg, which forms an inter-
esting feature in Colonial history. This place was once the strong-
hold of France in America, and has one of the finest harbours in the
world. It was well fortified; and a population of 20,000 souls
was contained within its walls. It was taken from the French by
4000 provincial troops, under Colonel Pepperall, in 1745. After-
wards Great Britain restored it to France. In 1758 it was again
captured by General Amherst. The place was defended by 3000
men, six ships of the line, and five frigates: in this action the
brave General Wolfe won an early distinction. The inhabitants of
the city were dispersed; and the British Government expended
£40,000 in blowing up the fortifications. The city is now occupied
by six families of poor fishermen; two stories of the hospital remain, as
do the foundations of the Governor’s house and other public buildings,
with much of the massive masonry of the bomb-proofs and bastions.
Among the ruins are seen fragments of exploded shells and other
missiles, mingling with the crumbling bones of the killed. Had
Louisburg continued to exist up to the present time, its abandonment
would not have been the less certain ; for the sea now flows within
its walls and overflows sites that were formerly inhabited. Its sub-
mersion is plain and distinct. The rock upon which General Wolfe
landed has nearly disappeared. The waves break against the south
wall, which they have undermined and thrown down. The higher
parts of the fortress afford shelter for sheep ; but each succeeding
tide flows freely into the northern side of the deserted city. The
lands westward also bear testimony to an extensive submergence.

Prince Edward’s Island.—The fertile Prince Edward’s Island is
situated in the Gulf of St. Lawrence, fifty miles eastward of the

1861.] GESNER—MOVEMENTS OF LAND. 387

Province of Nova Scotia. It is composed of red sandstone ; no
workable strata of coal have been found within its limits. Of several
sinkings of the earth noted by the writer during his geological survey
of the island, one of them merits attention for being more recent
than any other that met his observation. It is situated between
Lennox Island and Cascumpec, a deep and well-sheltered harbour.
The sea has here thrown up mounds of sand from the shallow water,
which are separated from the mainland by lagoons. The lagoon
between Richmond Bay and Cascumpec is upwards of thirty miles
in length. Cascumpec lagoon is a beautiful sheet of water, eighteen
miles long and a furlong in breadth, abounding im shellfish and
wild fowl; its mainland side is a dense wilderness, and this part of
the coast was explored in canoes paddled by Indians.

The harbour of Cascumpec is formed by an extensive peat-bog on
one side, and a long mound of sea-sand on the other ; it has sufficient
water to float the largest ships. The peat forms a perpendicular
wall, which was measured at low water, and found to be 19 feet
beneath the sea. It is also perpendicular above the water and
forms the shore to the distance of two miles and a half. This peat-
bog is composed of the common sphagneous plants interlaid with the
pine, hemlock, and other forest-trees and low bushes, some of which
are still in upright positions. There are no higher lands in the rear
from which this bog could have made a slide, nor any remaining
site from which it could have departed.

In the lagoon, the sea flowed, at the time of the writer’s visit, into
groves of maple, beech, birch, &¢c., which are constantly falling
down from the sea-water overflowing their roots. The marshes,
where they meet the water, are filled with fallen timber; and all taken
together presents a desolate picture of the changes that are still in
progress. This part of the island is very low and level; and, from
the gradual submergence of the land, the drainage of the country is
obstructed, and lands now capable of being cleared and cultivated,
will in the course of years be overflowed by the sea, unless the sub-
mersion should be arrested.

At numerous places on the shores of the Gulf of St. Lawrence and
on the coast of Labrador, deposits of sand and clay containing recent
shells and relics of marine plants are found at heights varying from 5
to 80 feet above the level of the sea. These elevated tracts are seen,
at considerable distances from the present shores, with notches worn
out of the rocks by waves and currents of water; there are also
limestones perforated by the Mytilus lithophagus, from which the sea
has long since been withdrawn. At some localities there are also
evidences of depression, similar to those already described.

Labrador, §c.—The Atlantic coast of Labrador and the Island of
Newfoundland present the same phenomena, although they are less
perfectly delineated by reason of the ice ; for ice-floes break down the
shore, and icebergs deposit mounds of sand, gravel, and boulders
along the sea-bord, the winter and summer aspects of which are
altogether dissimilar.

Conclusion. —From what has been stated, it must not be under-

388 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Apr. 10,

stood that these silent wndulatory movements of the land are con-
fined to the coasts and estuaries: they are manifest on the borders
of the rivers and the great lakes of Canada, and also on the tributaries
of the Mississippi. Slight shocks of earthquakes are common in
Canada and the United States ; butit does not appear, in the history
of those countries, that any material change in the relative levels of
certain tracts has been effected thereby. Admitting, however,
that earthquakes have been the cause of sudden sinkings and elevations
of the land, and which would produce anomalous results, there is a
slow and constant undulatory movement of the earth’s surface,
which no doubt acts as much on the ocean’s bed as upon the dry
land.

——_

2. On the Guotoey of the Country between Laxe Superior and the
Pacrric Ocuan (between the 48th and 54th parallels of latitude),
visited by the GovERNMENT Exprortne Exprpirion under the com-
mand of Carrarn J. Patuiser (1857-60). By James Hector, M.D.

(Communicated by Sir R. I. Murchison, V.P.G.S.)

[Puate XIII.)

ConTENTs.
Introduction. Group D.
Genera PuystcAu FEATURES. Group C.
SUPERFICIAL DEPOSITS. Group B.
Terraces of the Lake Superior Relation of the Cretaceous Series
Basin. on the West.
Superficial deposits of the Central Cretaceous Strata of Vancouver
Plateau. Island and the Gulf of Georgia.
Terrace-deposits of the Mountains. Details of the Strata at Na-
Terraces in California. naimo.
Age of the Terrace-deposits. Panxozorc Rocks of THE HAsTErN Axis.
Drift of the Pacific Coast. Silurian rocks.
TERTIARIES. SrructurE oF THE Rocky Mountains.
Cretaceous System. Physical Character.
Group F. Geological Structure.
Group E. THe Cascade RANGE.

Introduction.—In the spring of 1857 Her Majesty’s Government,
at the suggestion of the Royal Geographical Society, constituted an
expedition to explore the british Territories in North America lying
in the neighbourhood of the boundary-lne of the United States, and
stretching westward from Lake Superior. Public attention was at
that time directed to the nature and resources of the vast territory
which had been ceded to the keeping of the Hudson’s Bay Fur Com-
pany, as there was a prospect of its being to some extent thrown
open to colonization by the lapse of part of that Company’s rights.

Principally through the efforts of Sir Roderick Murchison (at that
time President of the Royal Geographical Society), General Sabine
(acting for the Royal Society), Sir W. Hooker and Dr. Hooker, and
of Mr. Ball (then Under-Secretary of State for the Colonies), the Ex-
pedition was organized and committed to the charge of Captain

by

MRC
, ERY: Me

Woods Mire keeps

‘is

| .

Quart Journ Ceol Sor VoL AVI, PL Xi

Section N°] General Section from the Pavific Occur to Hudson Bay, on a NE tine between Vancouver Island and York Factory.

Rocky Mountains,

faseade Nountarw.

Prairies.

Columbian Desert. rout Buirte

y fest
=———

Diagram -section of British N. America, shewing the Geolagiwal Structure from

=
Giccade = Mountauns.
=

Sel

g

=
2

L100. miles Vertical Scale

Distance

Lake Winipey

ctght times the

Hortcontatl. —

Eastern Accts Hudson Bay.

of the Strata at wanaimo, fiom observed Sections.

1

|4s00)

‘
3
Sf Che Mize Ur, wait te line of Seti. eu
= taney Hore Basin 3
at Sere Mt

Lake Winipeo

= Lake Win

Vertical +000 rt. p. inch
4000 |

Seale © to D Harizontal. 100 niles p. inch
Cue 2 ww

Soule Ate B Horizental 20 miles pinch Vertical 20,000 6p tnck
Hoe hs 3 -~ 4,000

4000

Druirter a Trap of Foot [hint Geven Sanllstone with Teygenin, Exar, Exo eye

Thorerannis S thin Gal smun (inch Sqruriusales with Inocerwnnek<aSunr of thal Ae Reyphle a. Fault

Catone with Wood Leterule oP Peonit Botnie anil

Cytherea TeonenaipSee Font Minit. 6

0 Riv Write Neweastle Ls.urul the Gaiion.e Newourtle cralsciinn 10 1t£ Douglas tonlorounn tee etry iMlaceyus Sartetaries with

Ac timutomerates ant false Tetted Suntrtoner.

Tiudeon Bay
—*

—#

REFERENCE

(Baetertars

wt Wert Slope a

oF

GEOLOGICAL MAP

of the Country between
LAKE SUPERIOK & VANCOUVER ISLAND;
By James Hector, UD

Routes of Cape Dalliserts Exploriny Expelition

Soperiae

\
Hrerrstcet u
ST at said Late epoatte ust Stope| Section

| b [aa Miocene ignite Basin

(SS Focenel™ Marine. [evpres Hille}

1 Dyer

| Cretaceous

WH sitale

fF Ea Lower

elle Lagrate

} strata of the
i Prairies

Disturbed Oretaceous strata of Rocky MY
loud Lignite yrsiup of Vancouver Laland.

| 7 Ese

=

Un es

SQ] Girhenivern us Limestone.

6 I Peromun timerune

2 {tisilurinn of Hudsore Bay, anit
J BR Sittin of tiniged:
\Murerian vf T..Superiors

& unl Scitate of Rockey Mountains

Metconanplite Rocks and Greniite-

mw
in (erntsd] Voleanic Rocks

The following AUTHORITIES core also amadted-
M8) Merle & Maven (ppa Missouri Richardson & Mint Miniper District

<t

Logan, Owen Higehy HL Superior Bauerman &tilmer [Grseade ME)

: = = 3 = Tae agar
Section of Cimoe Route bawen LMinipeg & LSuperior. E | aoa |
ars Ee ce — i GEOLOGICAL SKETCH-MAP OF
an 4 NANAIMO,
RE * Green Sandstone Vancouver Island.
Laurentian Anis 2 with Teigenla By James Hector, MD: 1

few castle Seam

eu

Yewoustle L.

§) Douglas L. }

ANAIMO

Seale oF Miler
ns b '
Tar of Comp B.

Cala Descanco I

i

Wes Vertaca,

Lake We

umo,from observed Sections.

Mountains.

R
k
AM gil Point.c.Gravel-stone with Wood. Islands off Fossil Point and

=E2S6 it) £. Douglas Coal-seam/trt/ &Argillaceous Sandstones with -

d:a.Faudt /?/ \e Conglomerates and false-bedded Sandstones.

1239 50" 123° 45"

eer L.Wirdipeg & 1.8: } BI

_ 2PaL® GICAL SKETCH - MAP OF 49°
eee NANAIMO, .
; : Vancouver Island.
Ream Aavts By James Hector, M.D. bs

©

2 ———————
er
SS Scale of Miles
= ; e _¢ _# Is
Var. of Comp.23°E.
AREFERENCE
atiary. Cala Descanso [

—ed. Shinale of West Slop
— Pritt “and Lalke-depost

Ja’ '

ve Lronite Basin. ee |

S/S? Marine. / Cypres hh

:
wae Cretaceous
ey strata of the }
| Prairies. =
fate ;

yved Cretaceous strata «
wWygnite group of Vance

iverous Limestone.

Bank

‘an Limestone. armas
: ues:

tur of Hudsor Bay, a
- - - - »
tam of L.Wintpeq.

<

am or L.Superter,
‘chists of Recl:vy Mount
: =,

— . -
_Drorplite Rocks and Gr

UTHORITIES are.als
. =ssouri | Richardson &

Superior, Bauerman &—

1861.] HECTOR—ROCKY MOUNTAINS, ETC. 389

Palliser, whose previous adventurous travels in that region had given
assurance of the ability and energy necessary to penetrate unexplored
country, and to preserve a friendly footing with the savage tribes
that were to be encountered.

I was selected by Sir Roderick Murchison to accompany this Expe-
dition in the combined capacity of surgeon and geologist; and, at
the request of Government, he furnished me with instructions as to
how I should turn to best advantage my opportunities for geological
research.

The more important results of my work I have now the honour
to communicate through him to this Society.

They have been accumulated during three years’ travel in wild
regions uninhabited save by Indians, or, at rare intervals, by little
communities of persons engaged in the fur-trade. Excepting in the
maps of Mr. Arrowsmith, which gave very correctly, on the whole,
the great general features of the region explored, embracing 33°
of longitude, and in some places 5° of latitude, nothing was known of
its topography; so that this essential to sound geological reasoning
had to be acquired step by step as the country was examined. I
therefore submit my observations only as the best I could make
under the circumstances, knowing that a re-examination of the
country with the aid of the topographical details which we now
possess would materially alter many of the views I have expressed.

Our previous knowledge concerning the geology of the interior of
British North America was confined to the observations of Sir John
Richardson, made during his three great overland arctic expeditions—
the first two with Sir John Franklin, and the last in search of that
lamented traveller. His published descriptions of the country he
passed through are models of minute observation and cautious in-
ference. To him we owe the first discovery of Silurian strata resting
on a primitive axis stretching to the north-west from Lake Superior
to the Arctic Ocean, and overlain by Devonian strata. He also
showed the Rocky Mountains, where he met them on the Mac-
kenzie River, to be composed of Carboniferous Limestone for the
most part, which is also their character, we shall find, further to the
south. From Elk River he brought home fossils which, although
from a group of strata which he classes as Devonian, yet in a foot-
note, on the authority of Sowerby, he says have quite a Jurassic aspect.
That he was right in the latter suggestion is rendered probable by
the recent publication of species of Ammonites by Mr. Hind, which
were procured from that locality by the fur-traders, and which
Messrs. Meek and Hayden consider to be of Jurassic age. Sir John
Richardson also described the existence of a great lignite-basin in
the valley of the Mackenzie River, which he classes as of Tertiary age.

The line of route, however, followed by Richardson did not, with
the exception of the canoe-routefrom Lake Superior to Lake Winnipeg,
and again at Fort Carlton on the Saskatchewan, touch on the country
which has been explored by this Expedition. With regard to the
canoe-route, I have added nothing to the researches of that traveller,
and to the still more minute observations of Dr. Bigsby, which were

390 PROCEEDINGS OF THE GEOLOGICAL SOCINTY. [Apr. 10,

some years ago communicated to this Society. In 1855 Mr. A. K.
Isbister communicated to this Society a useful and concise recapi-
tulation of what had been written concerning the geology of the
Hudson’s Bay Territories, without adding anything, however, to our~
knowledge of the central district with which I have principally to
deal. It is to Mr. Hind alone, who was in command of the Cana-
dian Expedition to explore part of Rupert’s Land, that I can refer
in confirmation of my observations in any part of the prairie-regions.
Mr. Hind in 1858 partially travelled over nearly the same ground as
that traversed by our Expedition during the previous summer, but
only as far as the elbow of the South Saskatchewan, and in regard to
all essentials our work agrees exactly*.

Mr. Hind’s report is valuable from his having had his fossils
examined by Messrs. Meek and Hayden, whose labours in the Upper
Missouri country and Western States since 1852 have given us most
of the knowledge which we possess concerning the classification of the
strata composing the northern part of the great American prairies ;
and to those gentlemen I shall have frequent occasion to refer.

Concerning the mass of the country explored, consisting of the
prairies within the British possessions and the Rocky Mountains be-
tween latitude 49° and 53°, and of the country westward to Fort
Colvile, I am not aware of anything having been published, except-
ing a few general remarks collected by Richardson from the botanists
Douglas and Drummond or from the fur-traders.

Concerning the geology of the Pacific Coast, in the neighbourhood
of the 49th parallel, there are very interesting notes scattered through
the various U.S. Senate-papers, by Mr. Gibb and Dr. Suckley, who
were employed in the survey for the Pacific Railroad. The former
gentleman is still working in that country, being attached to the
North-west Boundary-Commission. There is also a short notice of
the geology of Vancouver Island, by Mr. Bauerman, geologist to the
British section of the same commission, published in the Geol. Soe.
Journal for 1860.

GENERAL PHYSICAL FEATURES.

The prairie-country which I have principally to describe may be
considered as forming the northern portion of a triangular space con-
taining the plateau which occupies the central region of the North
American continent, having for its sides, first, the Rocky Mountains ;
second, the Laurentian axis or “intermediate primitive belt” of
Richardson ; and third, the Alleghany Mountains.

A low indistinct water-shed 850 feet above the sea at its lowest
point, and apparently undetermined by any disturbance of the rocky
framework of this basin posterior to the deposit of its more uncon-
solidated contents, follows a line sometimes north and sometimes
south of the 49th parallel of latitude (which is the Political Boun-
dary-line), dividing the waters which flow to the Gulf of Mexico from
those flowing to the Arctic Ocean.

* My first Report on the Geology of this district was dated December 14, 1857.
See Parliamentary Papers, June 18959.

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 391

The route of the Expedition starting from Lake Superior, after
crossing a spur of the eastern axis, traversed the northern part of
the plateau to the Rocky Mountains, and thence down the western
slope of the continent to the Pacific Ocean.

The Mackenzie River, rivaling in its proportions the Upper Mis-
sissippi, breaks the apex of this triangle, escaping through the Rocky
Mountains to the Arctic Sea; while the Saskatchewan and other
rivers of the southern British territory dilate into great lakes at the
western base of the Laurentian axis, through which they then escape
to Hudson Bay.

The Laurentian axis of metamorphic rocks with its fringe of
Silurian strata may be considered as stretching from Western Canada
to the Arctic Ocean, near the mouth of the Coppermine River, inaN.W.
direction ; but it sends off a spur, which encircles the western shore
of Lake Superior, and loses itself under the prairies of the State of
Minesota.

Lake Superior and Lake Winnipeg, according to the surveys
of the Canadian Expedition, have nearly the same altitude of
600 feet above the sea, while the rocky district that separates them
has double that elevation, or 1300 feet, above the sea; but this is in
many places increased to 1600 feet by the deposits of drift that will
be hereafter described.

The highest point of the great plateau that is in British territory
is to be found when, at the base of the Rocky Mountains, that chain
is intersected by the 49th parallel of latitude, where it is elevated
4300 feet above the sea. If followed into the United States to the
south, it is found to reach a still greater elevation along the base of
the mountains, until it merges with the great table-land of Mexico,
which has an altitude of 6000 feet. From the above point of inter-
section to the nearest point of the Laurentian axis, which is a line
from near the source of Belly River in a N.E. direction to Cumber-
land House on the Saskatchewan, the distance in an air-line is over
500 miles, and the difference of elevation of these two points gives a
mean slope of 6 feet in the mile. The general level of the eastern
base of the Rocky Mountains also declines rapidly to the north ; for
in latitude 51° 9’, at where the Bow River emerges on the plains, the
elevation is 3900 feet, and at where the Athabasca, the most southern
tributary of the Mackenzie, leaves the chain in latitude 53°12’, it is
only 3300 feet above the sea*.

The slope of this plateau is, however, far from being uniform, but
is broken by steppes which have been formed by the erosion of
the surface of the country, and which indicate different grades in
the elevation of the continent during later epochs. These steppes
are boldly marked, sometimes increasing the altitude of the prairies,

* As the Rocky Mountains are cut through by valleys almost to. the depth
of the plateau on which they stand, this depression of the chain towards the
north has a remarkable influence on the climate in some localities, especially
mitigating the severity of the spring months by admitting the influence of the
mild climate of the western sea-bord at a time when the eastern part of the
continent in the neighbourhood of the great lakes is still icebound.

392 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

as the traveller follows a westerly course, by an abrupt rise amounting
to 600 feet. They have avery irregular outline, and are cut through
by the river in many cases, so as to form isolated masses of broken
table-land. (See general section: Sections Nos. 1 & 2, Pl. XIII.)

The Rocky Mountains forming the western limits of the great
plateau rise from it very abruptly, the eastern ranges often present-
ing sheer cliffs 2000 to 3000 feet in height. These are, however,
cut by transverse valleys into which the superficial deposits of the
prairies penetrate, and have been preserved, more or less perfectly,
as terraces in the mountain-valleys.

The mountains formed of broken plications of strata, as will be
afterwards described, are disposed in parallel groups, the great valleys
in the length of the chain generally occupying anticlinal fractures.
The flexures have been more perfectly developed in the eastern part
of the chain than towards the central parts, where the mountains have
a massive cubical aspect, the strata having been fractured and up-
heaved rather than bent by disturbing agencies. This is owing,
no doubt, to the mineral composition of the strata,and not to any modi-
fication of the disturbing force; for, as the western slope is descended,
slaty rocks are met with, which again present perfect flexures. The
mean altitude of the Rocky Mountains between latitude 49° and
58° is about 12,000 feet above the sea, but there is a very singular
absence of marked peaks. The chain culminates in latitude 52°,
where the mountains are very massive and are traversed by profound
valleys, the heads of which are occupied by glaciers.

From the Rocky Mountains to the Pacific Ocean the country is
extremely rugged, resembling similar Silurian and metamorphic
regions in other parts of the world. It forms a great trough,
bounded to the west by the Cascade range of mountains, which
closely hugs the Pacific coast in this latitude. This range, which
is only rarely broken by valleys, and those of comparatively recent
date, runs like a wall 4000 to 5000 feet above the sea-level. At
intervals there occur great conical mountains, such as Mount Hood,
Mount Baker, and others, which rise to 10,000 or 12,000 feet, and
from their isolation, being perfectly unconnected, except by the
lower range, they present a very grand appearance when viewed
from the coast. Owing to the great fall of the rivers, the narrow
valleys, and the rapid erosion having continually carried on the re-
arrangement of the superficial deposits, the grades in the elevation
of the continent cannot be so well discerned on the western slope as on
the eastern, although these deposits are found to be greatly developed.

After this brief sketch of the physical features of the country, I
now proceed to describe the different strata, reversing the order of
their deposition.

SUPERFICIAL DEPOSITS.

These are very extensively developed in every part of the region
explored; and their classification involves very interesting conclusions
respecting the changes of level of the continent, both posterior and
anterior to the great northern drift.

1861.] HECTOR—ROCKY MOUNTAINS, ETC. due

Judging from the altitudes at which erratics are found to be di-
spersed, the continent must have been depressed at that period
beneath a sea in direct connexion with the Arctic Ocean to the
depth of nearly 3000 feet ; and since then, during its gradual emer-
gence, this region of North America has received its present form of
surface by denudation,—-first, as effected on seacoast-lines, and lat-
terly by the coast-lines of great inland lakes, which, it will be shown,
though still existing, were previously of much greater dimensions.

The superficial deposits during and posterior to the Drift are so
different on the opposite sides of the Rocky Mountains that they
must be treated of separately, whilst those anterior to that epoch
will be found to have a common character.

Terraces of the Lake Superior Basin.—In ascending the Kaminis-
toquoia River for a considerable distance above the Kakabeka Falls,
the country is covered by a deposit of red marl-earth which forms
the high terraces of the river. Thus opposite to the mouth of White
Fish River there are three distinct terrace-levels of 20, 60, and 90
feet. At some distance back from the river still higher terraces
occur, belonging to this class of deposits, which must be considered
as of more recent age than the true drift. Sir William Logan de-
scribes one at the height of 331 feet above Lake Superior. The
great deposits of sand and gravel which rest on the highest levels of
the axis, and are first met with at Dog Portage, belong, I think, to
the period of the Drift, and will be referred to in the next group.

Superficial Deposits of the Central Plateau.—The steppes of this
great slope may be naturally divided into three groups having dif-
ferent ages and circumstances of deposition, and boldly marking three
distinct Prairie-levels. (See Sect. No. 2, Pl. XIII.) To the most re-
cent of these belong the low prairies which surround Lake Winnipeg
and the lakes of that group, including the marshy country to the west
of Manitoba Lake. This forms the First Prairie-level. In the vicinity
of the Red River Settlement, its composition is of argillaceous marl,
with a deficiency of sandy matter, and it is invariably stratified
in thin layers. Underlying this at various depths from the surface,
is a bed of stiff clay, which forms the immediate margin of the river
at many places. The upper layers of this deposit contain leaves and
fragments of wood and reeds, and the whole is undoubtedly a fresh-
water deposit, indicating a time when the Winnipeg group of lakes
covered a much more extended area than at present, the gradual
deepening of the rocky channels through the eastern axis having
increased the drainage in modern times.

The surface of this deposit is about 75 to 100 feet above Lake
Winnipeg, but it slopes gradually from the west, and at Pembina
Mount, near St. Joseph, is at least 100 feet higher. To the east of
Red River, in descending the Winnipeg River, two well-marked
levels were observed which belong to the group of extended lake-
deposits. Thus below the Seven Portages that river flows through a
smooth channel, and the banks are composed of a white marl-earth ;
the river being at first only slightly depressed, but soon from its
rapid descent, while the level of the deposit remains the same, the

ut PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

banks become high. At the Rat Portage, this terrace, which is 150
feet above Lake Winnipeg, retires from the river on each side, and
is replaced by another at an altitude of only 75 feet, through a cut-
ting in which the river flows to its mouth at Fort Alexander. This
ancient lake-bottom extends south of the 49th parallel into the
American State of Minnesota, and everywhere presents a rich level
prairie, only broken by slight gravel-ridges which have formed
shoals in the ancient lake, or by patches of the magnesian lime-
stone beds which crop out into the plain, such as at the Stony
Hills, east of Fort Garry, which must have been a rocky island at
one time.

The banks of the lower part of Rainy River are composed of rich
alluvial deposit of a light-grey colour, containing a large proportion
of white sand. It is distinctly stratified, and has without doubt
been formed by an extension of the Lake of the Woods back towards
Rainy Lake. In the upper part of Rainy River, the banks are high
and terraced, and boulders show that at this level there is also a
deposit of true Drift.

At Pembina Mountain, the eastern limit of the Second Prairie-
level forms an escarpment measuring 250 feet above the plain at its
base. From the point where it crosses the 49th parallel, it sweeps
to the north-west and assumes a more gentle slope, being broken up
into three or four subsidiary terraces. It then meets the Assine-
boine River near the mouth of the Souri, and is continued to the north
by the high grounds that lie to the west of Manitoba Lake from Riding
Mount to the Basquia Hills, which, however, rise to the full height
of the level—that is, to 1600 feet above the sea. Below Fort a la
Corne the banks of the Saskatchewan are described as suddenly be-
coming reduced from the height of several hundred feet to a slight
elevation above the river, showing that it is at that place where the
eastern limit of this level meets that river. The prairies of the
Upper Assineboine, the Qu’appelle River, and those along the Sas-
katchewan, from Fort 4 la Corne to the elbow on the south branch,
and also up as far as the longitude of Fort Pitt on the north branch,
all belong to this level, which also extends to the base of the Great
Missouri Céteau. The mineral composition of the superficial de-
posits of the Second great Prairie-level is very different from
that of the first. Sand is the predominating ingredient. Thus at
St. Joseph, where the banks of the Pembina River present a fine
section of it to its base, the material is a coarse red sand, with
gravel and boulders. There are no signs of stratification in any
part of this deposit as seen at Pembina Mount, but further west,
where it assumes a light-grey colour, and contains a considerable
quantity of lime, it is imperfectly bedded. Near Fort Ellice, and
at many other parts of the district to the south and west of that
place, this deposit is formed wholly of fragments of the under-
lying Cretaceous shales. At Long River, Forked Creek, and many
other places, this deposit was observed to form only a very thin
coating to the Cretaceous rocks. Notwithstanding that the prai-
ries of this level are often cut to a great depth by the rivers and

ee ea —

id

1861.] HECTOR—ROCKY MOUNTAINS, ETC. 395

ereeks, very little can be learnt of its nature at different points, as
slides in the banks of the gulleys are rarely seen. At Fort Ellice
the valley of the Assineboine is 240 feet deep, and about 100 feet of
that is composed of this drift-deposit resting on the Cretaceous beds.
In the Qu’appelle Valley, near the Mission, a slide exposed the
deposits beneath the plane to the depth of 250 feet, showing it to be
composed of stiff sandy clay of light-red colour, with patches of blue
clay and gravelly beds. On the whole, the character of this level,
as far as regards its mineral composition, is variable and local.
Boulders are tolerably plentiful all over its surface, but occur in
greatest quantity on the sides and summits of ridges and mounds,
which rise in groups to the height of from 50 to 80 feet. Im-
mense outliers of a still higher level occur, attesting the immense
denudation which has taken place; these generally rise from 1400
to 1600 feet above the sea, which latter is the height of this level
at the base of the Grand Coteau, Eagle Hills, and Thickwood Hills,
all of which form the eastern limit of the next great steppe. (See
fig. 1.)

Fig. 1.—Section 16 miles above the Elbow of the South Saskatchewan,
showing the junction of the Drift and the Cretaceous clays at the
base of the Third Prairie-level.

a. Drift. 6, Septaria-clays (Upper Cretaceous).

These outlying patches occur along two lines parallel to the general
contour of Lake Winnipeg and that of the next higher level to the west,
and were doubtless continuous ridges until cut through by the dif-
ferent river-valleys. Thus overhanging the lakes, we have the Pas,
Porcupine, Duck, and Riding Mounts ; and to the west, a line of which
the Touchwood Hills, Moose and Turtle Mountains form the prin-
cipal points. These have all a common character, rising gently to
an ill-defined table-land from the west; while their eastern aspect
is extremely rugged, presenting irregularly deposed ridges of coarse
sandy drift highly charged with boulders. This steep escarpment
is generally densely wooded, and encloses numbers of small lakes.

The eastern limit of the Third great Prairie-level is met with at
the Grand Coteau, Eagle Hills, and Thickwood Hills, and is only cut
through by the channels of the north and south branches of the
Saskatchewan ; while all the other rivers of the eastern plains, such
as the Souri, Assineboine, Qu’appelle, &c., have their sources short of
it. I have stated the prairie at the base of this third level to have
an elevation of 1600 feet above the sea, and a depression of the
continent to this extent would be sufficient to submerge the eastern
Laurentine axis between Lake Winnipeg and Hudson Bay, or at
least to convert it into a mere chain of islands. The eastern coast-

396 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

line would then leave the Rocky Mountains in latitude 56° N.,
near Peace River, and would follow what is now the water-shed
between the Saskatchewan and the rivers more to the north, till it
reached the 107th of longitude. From this point the Thickwood
Hills, Eagle Hills, and Thunder-breeding Hills would form tke
headlands of a great bay into which poured the waters of the two
Saskatchewans, at that time independent rivers debouching where
they now make the acute bends known as their ‘‘ Elbows’’. The coast-
line was then continued to the south-east, forming the céteau that dips
between the Missouri and St. Peter’s Rivers. As seen from a dis-
tance when travelling in the low plains, this great steppe appears as
a range of blue hills with a smooth undulating outline. On ap-
proaching it a gentle ascent is accomplished for many miles, after
which an abrupt rise of from 400 to 600 feet has to be effected,
generally in from 4 to 6 miles. The surface of the slope is extremely
rugged, and has evidently been worn into pot-holes, ridges, and
conical mounds by the action of water on the soft clay strata of the
Cretaceous group. Everywhere the slope is thickly strewn with
boulders, all derived from the Laurentian chain to the east, or from
the Bird’s-eye Limestone which rests on the western flank of that
axis.

Near the elbow of the North Saskatchewan a remarkable group of
boulders of this kind of limestone, of enormous size, crosses the
country in a line parallel with the céteau to the west. This line
has been observed at pomts 30 and 40 miles apart. They occur as
great angular masses, consisting of several of the beds of limestone,
the coherence of which being very slight proves that they must have
been stranded without any great violence. One of these masses con-
tains over 3000 cubic feet of stone, and rests on the plain obliquely
with its south-western angle buried in the soil (see sketch, fig. 2).

Fig. 2.— Boulder on the Plains south of Carlton.

More to the west than this is a line of sand-hills, which has evi-
dently marked a coast-line, although their original position may now
be much altered, since they are still wind-blown as during their
first production. They have a clear relation to the ancient level,
and are found at the same altitude over such a stretch of country,
always at a little distance from the base of the escarpment, that there

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 397

ean be no question as to their origin. Similar sand-hills were ob-
served on the Souri River at the base of the Second Prairie-level,
which must have been formed on the shore of the extended lake.

The resemblance which the plains along the base of this great
steppe bear to the shore of Hudson Bay at the present time may be
judged of from the description given by Sir J. Richardson, who says,
«<The western shore of Hudson Bay between latitude 56° and 58°
is flat, and the depth of the sea decreases very gradually on approach-
ing them. In seven fathoms of water the tops of the trees are just
visible from a ship’s deck. Large boulder-stones strew the beach,
and form shoals even at the distance of five miles from the shore, which
are very hazardous to boats.’ in proceeding up the river from
this coast, he says that after a tract of level country “the banks”
(consisting, he before mentions, of drift-clay and boulders) “rise
from a very narrow river-channel to an elevation of very nearly
200 feet. Their outline is broken into conical eminences by short
ravines, which open into the river at right angles. These banks have
exactly the same form and constituent parts as those which occur on
the confines of Lake Winnipeg and the Saskatchewan.” As he made
the latter remark in allusion to the nature of the underlying rocks
at the two localities without reference to the drift, it is all the more
valuable for the purpose of proving this similarity, which is so
striking between the present state of the coast of Hudson Bay and
the ancient coast-line along the base of the Third Prairie-level. In
the rugged district of this steppe there are enclosed numerous lakes,
some of great size, and all, without exception, more or less impreg-
nated with salts, of which sulphate of soda is the predominating
ingredient. in autumn after the dry summer, these lakes are fringed
with erystals, and the soil in many places is covered with a white
efflorescence. Whether these salts are derived from the superficial
deposits of the ancient coast-line or from the Cretaceous clays, I am
unable to say; but the position of the salt-lakes, generally at the
same altitude, inclines me to the former opinion.

The Laurentian axis is covered with a great deposit of drift, con-
sisting of coarse red sand, with many large and small boulders. This
deposit forms a flat swampy plain, well wooded towards the west, but
towards its eastern margin, as at Cold Water Lake, worn into deep
dry gulleys and round pot-holes without any exit. The thickness
of this deposit is from 200 to 300 feet, and the highest point of it
is about 900 feet above Lake Superior, or on a level with the plains
near Carlton. Glacial seratchings were distinctly seen at many
parts of the axis. The direction is generally north and south.
Hardly a surface in the granitic tracts did not present distinct
scratches. They were seldom, however, to be observed on southern
exposures of rock-surfaces if these sloped much; but the more
surfaces with northern exposures sloped, the better they seemed
to be marked.

As will be seen from section No. 2. Pl. XIII., in rising to the sur-
face of the third steppe we have the plains composed of the Cretaceous
strata with only a very thin coating of Drift, which has always a local

VOL, XVII.—PART I. 25

398 PROCEEDINGS OF THE GEOLOGICAL socieTY. _—_{ Apr. 10,

mineral composition, corresponding with that of the underlying
strata, without admixture of materials carried from a distance further
than a sprinkling of erratic blocks, of small size, and only to be
found crowded on favourable spots.

These consist almost entirely entirely of fragments of metamorphic
rocks, limestone being very rare.

I have not remarked the ordinary erratics at a greater altitude than
3000 feet; but at 3700 feet above the sea and 50 miles from the
Rocky Mountains, there occurs a very extraordinary group of blocks
of granite, resting on a high plateau formed of sandstone strata.
These blocks are of great size, one having been estimated to weigh
250 tons. Although lying in a line miles apart, they seem to consist
of the same rock—viz. a mixture of quartz and red felspar, the latter
predominating, with only fait traces of mica disseminated in very
minute flakes. They present smooth surfaces, although in general
they are rhomboidal in form. Some of them are cracked into several
pieces, which are quite detached, but are evidently parts of the same
block*.

If these blocks were derived from the granitic belt to the east, as I
believe all the erratics of the prairies have been, they must have
travelled at least 400 miles. From the fact, however, that they are
beyond the western verge of the Drift, and that the boulders were
found, as a rule, to diminish in size in that direction, it maybe that the
presence of these blocks is due to very different agencies,—different,
at least, in the time of their occurrence. No granite was observed
on the east flank of the Rocky Mountains within British territory,
but the Trois Butes, south of the 49th parallel, are said to be com-
posed of granite, and also the Black Hills; but both of those lo-
calities are much to the south of where those blocks occur.

The surfaces of the higher plains are in some localities traversed
by profound rents, resembling the valleys of great rivers, but which,
after running for several miles, are generally found to be closed at
both ends. They are often occupied by deep lakes of salt water, de-
pressed 200 feet to 300 feet below the plain, and from 500 yards to
a mile in width. The great coulées in the neighbourhood of the
Ear Hills, south of Battle River, are the best examples of these ;
but they are found in many other localities. It is difficult to con-
celve that they are due to erosion alonet.

Before leaving the superficial deposits of the prairie-country, it is
necessary to notice the great river-valleys which traverse it, and

+ For mention of a similar phenomenon, see Hooker’s ‘ Himalayan Journals,’
vol. i. p. 201.

if The ravines mentioned by Sir Charles Lyell, in his Second Journey in the
United States, p. 25. vol. ii., as occurring in the cretaceous and tertiary strata of
Georgia, seem to be very similar to them. He says, that when the woods are
cleared from the country, the sun, acting on the unprotected surface of the argil-
laceous strata, produces cracks that are soon enlarged to great gulleys by the
torrents of rain that fall. We may suppose that on the Saskatchewan, where there
is only a small quantity of rain, the -winter’s frost effects the same result, but
with this difference, that the successive landslips, remaining unmoved, at last form

such a gentle slope that vegetation can retain its hold, so that the rent is finally
represented by a symmetrical valley.

1861. ] HECTOR—-ROCKY MOUNTAINS, ETC. B99
which all point to a time when the rivers exercised a more powerful
influence than now; as even small streams, such as Battle River,
flow through valleys from 150 to 250 feet deep, which have been
partially refilled with stratified deposits. The sides of these valleys
are in general as regular and formal as those of a railway-cutting,
excepting where the nature of the strata causes frequent slides, or
harder beds give rise to a cliff-structure. The fiat alluvial bottoms
of these valleys are often four or five times the width of the river
which winds through them. and whieh is hemmed in by secondary
banks 30 to 40 feet high. The silt and alluvium are in general re-
gularly stratified, and almost every river-point contains one or more
lagoons, showing the frequent, though slow, change in the river-
channel.

Terrace-depesits of the Mountains.—At the distance of 90 miles
from the Rocky Mountains, the valleys of the rivers flowing to the
east commence to exhibit terraces composed of rounded fragments of
quartzite and limestone, such as would form the rounded shingle on
a rocky shore. At the Rocky Mountain House, where these terraces
first attracted my attention in the winter of 1857-58, the North
Saskatchewan has excavated a valley in the Cretaceous strata, whick
varies greatly in its width, sometimes being hemmed in by perpen~
dicular cliffs of sandstone, and sometimes sloping gently back to the
elevated country on either hand where the strata had been less
able to resist the erosion.

Yn this valley there are three terraces extensively developed at 20,
60, and 110 feet above the water-level*. Until we approach close
to the mountains these terrace-deposits are confined to the valleys
of the larger streams, but gradually they spread out, and at last cover
the whole country along the base of the mountains, filling up the
hollows and valleys of the outer ranges to the depth of several
hundred feet. This feature was observed at every point where we
approached the mountains from the east, from the 49th parallel north-
wards, and indeed was even better marked on the Athabasca River
than on any of those further south. Judging from the accounts of
American explorers, these terraces extend along the base of the Rocky
Mountains all the way south to Mexico.

One hundred miles east of the mountains, in latitude 49° 30’ N.,
shingle-beds are found to cap the Cyprés Hills, which have an altitude
above the sea of 3800 feet, or nearly the same as that of the base of
the Rocky Mountains. The Cyprés Hills are nothing more than the
western extremity of the great Missouri cdfeau, which, curiously
enough, here presents an escarpment to the west, and is separated from
the mountains by a tract of flat arid country of the above width. This
coteau is composed of Cretaceous and Tertiary strata, which have re-
mained as a dividing ridge, from the denudation having acted to the
north and south of the line which it marks. It is on the west and
south exposures ef these hills that the shingle ogcurs, formed inte
terraces like those along the mountains.

These are not to be classed, however, with the river-terraces, which

* These are roughly introduced in fig. 7. p. ae
ZEZ

400 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

are of much more recent formation, having been derived from the
deposits along the base of the mountains *.

This may not only be inferred from their relative position, but also
from the composition of the terraces themselves; for, although the
pebbles are the same in all, those in the valley-terraces are well
cleaned and mixed with sand, while in the terraces along the moun-
tains and on the Cyprés Hills they are often encrusted with white
calcareous matter. This sometimes increases so as to form a perfect
cement, so hard as to allow of the fracture of the pebbles before that
of the matrix, just as is seen in some ancient conglomerates Tf.

On approaching the Rocky Mountains the extreme regularity with
which these deposits have been terraced by retiring waters at once
attracts attention. At the place where Belly River leaves the moun-
tains, in latitude 49° 34’ N., Capt. Blakiston measured three of these
terraces, and found that they were elevated 61, 152, and 202 feet
‘above the river-level, which at that point, according to his measure-
ment, is 4024 feet above the sea. He describes them as being ‘“‘ very
marked, appearing as a succession of steps from the level of the river
to the plain above, often in sight for miles and running horizontally.
‘The tread of the step is of variable width, but the rise is nearly
always abrupt and well marked.”’ From the regularity of these
embankment-lke terraces in the valley of one river, he named it
Railway River (Further Papers, Palliser’s Expedition, 1860, p. 68).

On Bow River they are also well marked, and there I measured
four at the altitudes above the river-level of 380, 140, 170, and 240
feet, and traces of one still higher at 350 feet. The valley of Bow
River within the mountains is narrow and tortuous for the first
twelve miles, and in this part of its course the terraces are hardly
preserved. Above this point, where it occupies one of the expanded
horizontal valleys conforming to the strike of the strata, they are
again enormously developed. Even on gaining the Vermilion Pass
the only steep climb is at first, up the face of these terraces for 150
feet; and then a gentle slope leads to the height of land.

The valley of the North Saskatchewan is much wider and more
direct within the Rocky Mountains; and there we have not only
these terraces remarkably developed, but also their mineral compo-
sition much altered, partaking of what will be found to be their
character on the western slope of the mountains. At a similar
place, with respect to the mountains, to where the terraces were
measured on Bow River, four were estimated to have an altitude of
25, 70, 180, and 300 feet above the North Saskatchewan. The
shingle, cemented into a hard conglomerate, was here seen to rest
on the edges of the contorted strata of grit and shale with thin

* In latitude 42° at the base of the Rocky Mountains near Fort Laramie,
Hayden describes similar “ deposits of coarse conglomerate, 50 to 150 feet in
thickness, formed since the scooping out of the present river-valleys.”—Proc.
Acad. Nat. Sci. 1858.

+ Darwin says of the shingle-formation of Patagonia, “The pebbles are im-
bedded in a white, gritty, caleareous matrix very like mortar, sometimes merely
covering with a whitewash the separate stones, and sometimes forming the greater
part of the mass.”—Geol. of §. America, p. 19.

1561.] HECYOR—ROCKY MOUNTAINS, PTC. 401

seams of coal. Within the mountains the terraces expand so as to
form level prairies along the North Saskatchewan, of which the
Kootanie Plain is the principal. It is many miles in extent and
composed of shingle and incoherent sand, the widest terrace being
100 feet above the river. The river is, however, skirted by terraces
at still higher levels, especially on the south or right side of the
valley. Above Pine Point the calcareous matter of these terrace-
deposits so increases as to replace altogether the pebbles, and they
are often composed of fine gritty calcareous mud of glistening white-
ness. If followed into the higher valleys, they become confused with
the detritus of ancient glacier-moraines, which, however, are easily
distinguished by the angular blocks which they contain.

On the Athabasca River, at fifteen miles from the mountams in
a direct line, the terraces were found at 15, 100, 210, and 370 feet
above the river-level. Within the mountains, this valley, which is
more dilated than even that of the North Saskatchewan, has also the
terraces better developed than I have elsewhere observed them on
the east side of the chain. fhe river moreover dilates into extensive
lakes at different points of its course, and there the rearrangement of
the material of the terraces is seen to be going on; the water sepa-
rating the calcareous mud from the pebbles, while the winds, which
are extremely violent in this valley, sift out the fine sand and pile it
in tracts of sand-dunes which cover large areas.

The terraces may be considered as ranging on the east side of the
Rocky Mountains from 3500 to 4500 feet above the sea. Wherever
they prevail they support a growth of a peculiar sturdy pine which,
in common with the Banksian Pine, is known to the Hudson Bay
Company’s hunters as the Cyprés *.

Often the surface of a terrace is quite free from timber, the trees.
being easily thrown out of the loose gravelly soil, and then it is ge-
nerally clothed with ‘‘ bunch-grasst,”’ which at once catches the eye
as different from the grasses of the eastern plains. The country occu-
pied by the terraces is easily passed through, as the forests are there
free from underwood, and the only obstacle to the traveller arises
from his having so often to make a steep descent to the base of the
deposit, which is cut through by every little stream, and then to
climb again the opposite bank. When passing along the side of a
valley, the numerous cross gulleys due to this cause would render the
construction of a road a very difficult matter, although nothing could
be firmer or more level than the surfaces of the terraces themselves.
This remark applies equally to the valleys on the west side of the
Rocky Mountains, where the terrace-deposits have a much greater
development.

Terraces of the Western Slope.—All the valleys between the Rocky
Mountains and the Pacific coast lower than 4000 feet above the sea

* This pine is allied to the Pinus inops of the Atlantic bord and to the P. con-
torta of the Pacific, and yet has distinctive characters from either, It has been
proposed to call it Pinus Saskatchewensis, Hooker.

+ Festuce of various species. The grass on the eastern plains consists of varie-
ties of Chondrosium (Blodget’s ‘Climatology of the United States,’ p. 451).

402 PROCEEDINGS OF THE GEOLOGICAL sociery. { Apr. 10,

are found to be more or less occupied by deposits which are terraced
with greater regularity.

On descending the western slope, these deposits were first observed
in the lower part of the valley of Vermilion River, where they are
formed of the same glistening, white, calcareous mud that was seen in
the valley of the North Saskatchewan ; but it is in the wide valleys
of the Kootanie and Upper Columbia Rivers that these terraces are
best developed in the Rocky Mountains. These rivers ran in oppo-
site directions through the same great valley which lies parallel with
the mountain-axis for nearly 250 miles, and which throughout is
skirted by terraces forming a succession of platforms, often rising to
600 feet above the river. These extend into the side-valleys, pre-
serving their horizontal character, but their composition is often
changed. At various points these deposits were seen to be distinctly
stratified, and in some cases they must have been disturbed between
the time of their formation and that of their being finally moulded
into terraces. Thus where the Kicking-horse River joims the Colum-
bia, and where both valleys present perfect terraces at five different
levels, the highest, forming a wide shelf 540 feet above the river,
the appearance which is exhibited in fig. 3 was observed, where
the stream has worn away the bank.

Fig. 3.—Terraces in the Valley of Kicking-horse River, Rocky
Mountains.

Shingle.

Terrace, —

Moist sand,
Terrace.

Calcareous mud.

a
oO
60 feet.

Terrace.

Slate-rock.

The erosion of these deposits, and the production of steep and
quickly succeeding terraces (both being processes which may have
been simultaneously effected on successive shore-lines either of the
sea or of inland lakes) have been much more perfect in the valley of
Columbia, as far south as latitude 51°, than in the remainder of the
Columbia valley, which extends for a degree further to the south,
or throughout that portion of the same great trough which is oc-
cupied by the Kootanie River; for there the deposits remain com-
paratively undisturbed, and form great stretches of prairie, only
cut through by a narrow but deep channel for the river. The
change of appearance in the valley from this cause is very abrupt
and striking. North of latitude 51° the terrace- -steps succeed one
another rapidly, with the tread, or horizontal surface of the step,
narrow and furrowed; and the traveller’s progress is here impeded
by the dense growth of forest of a northern type, consisting of varie-

1861.] HECTOR—ROCKY MOUNTAINS, DTC. 403

ties of Spruce-fir for the most part, with dense underwood; but on
passing south of the slight bend of the Columbia, the tread of the ter-
race-steps commences to expand into wide level plains, dotted with a
forest of the sturdy Pinus ponderosa or the gigantic Laria occiden-
talis, both of which are trees that find their maximum in Southern
Oregon. The outlines of the terraces still preserve the same extreme
formality and steepness of slope, but on their level surface a rider can
gallop in almost any direction, so free is the forest from underwood.
Sometimes the trees are entirely wanting, leaving great tracts of open
plain embosomed in the mountains, forming the camping-grounds of
the Kootanie and Flat-head Indians, on which they raise the large
bands of horses for which they are famous amongst all other Indians,
the dry soil and nutritious bunch-grass producing a breed of superior
hardihood and swiftness.

In descending the Kootanie River from the Tobaco Plains * to
Colvile the country is rugged in the extreme, and these terraces are
met with wherever they have been sheltered from recent erosion in
valleys of unusual width or in recesses of the more narrow ones.
On reaching the belt of country where schistose and metamorphic
rocks prevail, the pebbles are often composed of greenstone, quartz,
and the other vein-rocks of the strata which they overlie. On reaching
the lower part of the country near Colvile, the terraces are still found
in all the valleys, not only at moderate elevations but also high up in
the mountains. Thus the Columbia at Fort Colvile, in latitude 48°
34’, is 1000 feet above the sea, and terrace-deposits were observed on
the sides of the valley at least 1200 feet above the river-level.

The great Columbian Desert and the Spokane Plain are both
covered with the same deposits of shingle, resting, in the former case,
on the great lava-floes, and, in the latter, on granite and metamorphic
rocks. The Spokane Plain, which is of comparatively limited extent,
has its margin beautifully terraced, repeating on a grand scale the
same phenomena as may be observed on the shore-line of a shallow
lake after the summer-drought. At old Walla Walla, where the
Columbia River passes from a wide and fiat sandy desert to break
through the profound rocky cazon of the Cascade Range, the whole
country is covered with light blown sand, which renders it almost
uninhabitable, being swept in clouds by the high gales that constantly
blow either up or down the river through this wonderful chasm.
Here in an ancient lake-bottom have been found the remains of a
Mastodon by some American explorers.

To the west of the Cascade range of mountains along the Pacific
coast, terraces of shingle prevail as in the interior. Also on Vancouver
Island they were observed near Nanaimo. Near Fraser River and
Puget Sound they are very well marked, and at the latter place occur
the “‘ Mound-prairies,”’ which, however, I only know of by report.
These are level surfaces of terraces free from forest, and covered with
lines of conical mounds, 10 to 20 feet high, said to be formed of

* The term ‘‘ Tobaco Plain’ should proper’y be only applied to a little plot

near the Kootanie Trading Post, but we have thought it advisable to extend the
name to all the large plains along the Kootanie River near lat. 49° N.

404 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 105

boulders piled on one another and resting on the surface of the
shingle.

Terraces in California.—Before leaving these shingle-deposits,
which are so largely distributed throughout the mountain-valleys
of British North America, I may mention that in California I found
these terraces ranging on the western slope of the Sierra Nevada,
at least to the height of 3000 feet, and there they are extensively
worked by the hydraulie method for the sake of the gold they con-
tain. At Nevada City, and also on the Yuba River, I saw deposits
of this shingle-conglomerate, 200 and 300 feet in thickness, ac-
tually being washed off from the face of the country by this power-
ful means, which consists in delivering water under great pressure
against the face of the eliff, from nozzles luke those of a fire-engine.
The supply of water for this purpose is in the hands of companies
separate from those that conduct the mining, as it is often brought
through tunnels and over high-level aqueducts from remote and
uninhabited regions. The particles of gold are dissemimated through-
out the whole deposit, but the richest washings are frem its base,
where a pink pipe-clay, technically known as “ pay-dirt,” rests on the
* bed-rock.” The whole water, with the material washed out of the
cliff, is directed through long troughs called ‘ flumes,” which are con-
structed of wood, lke mill-leads, often continuously for six or seyen
miles. The large stones are thrown out, as they pass, by men with
shovels, to save the wear on the bottom of the “flume,” while the
finer material is carried on by the rush of water, and passes over
frequent eross bars ealled “ ripples,” where a little mercury is plaecd
to entrap the gold by amalgamation. At Nevada City, where the
coating of shingle-deposit has thus been cleared from the surface of
the coarse-grained and soft granite which underlies it, gigantie masses
were exposed on what had once been the rugged shore of an inlet,
just as may be seen on a waterworn coast of the same material at
the present day. In California fragments of wood are found
throughout the shingle mm abundance, often carbonized, but in
general silicified into a substance exactly resembling asbestos. In
the sand and conglomerate of the Kootanie Valley I found fragments
of wood of similar appearance.

As my observations in California should not properly be introduced
in this paper, I shall leave them for another opportunity, the object
of my having mentioned them being to point out the great similarity
between the superficial deposits of the great gold-country and those
within the British territory further nerth, which encourages me to
assert that the whole country up to the Kootanie River and the base
of the Rocky Mountains, wherever the ancient terraces prevail resting
on Silurian or metamorphic rocks, will be found to be auriferous.
In my party in 1859 I had an expert ‘“ washer” who had been at
the Californian mines; and he frequently got “colour,” as a faint
trace of gold is termed, by merely washing the gravel from the beds
of the streams, without any regular “ prospecting” or “ digging.”
The discovery of what are among the richest “‘ pan-diggings ” on the
Pacific coast in the Schimillcomeen Valley, and the existence of

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 405

gold-mines worked since 1855 on Clark’s Fork, half a mile north
of the boundary-line where it meets the Columbian River, prove
that the belt of auriferous country in California and Oregon is con-
tinuous with that of Fraser River; and there is no reason to doubt
that in a short time the rugged and unexplored country which forms
a triangular region north of the boundary-line, and is drained by the
waters of the Upper Columbia and Kootanie Rivers will be overrun
by prospectors, and then by active gold-miners, just as the western
part of British Golumbia has been within the last few years *.

Age of the Terrace-deposits.—The evidence we have respecting the
age of the terrace-accumulations is very imperfect. There can be no
doubt that those occupying the valleys of the Rocky Mountains, being
furthest from the coast and at the greatest elevation, are the most
ancient, and that from the time of their deposit till now the rear-
rangement of the same materials has been carried on during the
gradual uprising of the continent.

The shores of the intricate channels and inlets on the Pacific coast
of British North America, if elevated from the sea, would present but
slight difference from sides of the narrow valleys in the Rocky Mount-
ains at an altitude of 3500 feet. Whether the continent was ever in
later times depressed to that extent in the mass, or whether the
central upheaval has been much greater than that along its margin,
is a consideration of great importance, and could perhaps be settled
by ascertaming to what altitude the terraces can be traced on the
Cascade Mountains.

The existence of marine Tertiaries along the coast, supposed to be
of the same age as those in the eastern prairies, and also within
the Cascade Range at slightly greater elevation and sometimes over-
flowed by the lava from those mountains, would seem to indicate that
the elevation has been very unequal; or, in other words, that the
Tertiary formations along the Pacific coast have hardly been raised
at all, while those in the interior are elevated several thousand feet.

On the eastern plains we have marine and other Tertiaries at an
altitude of about 3000 feet above the sea, and Hayden describes
them as “in all cases undisturbed, and not unfrequently resting on
the upturned edges of azoic and granitic rockst.” But in the
prairies these Tertiaries, along with the Cretaceous strata on which
they generally repose, have been enormously denuded, and are
found merely as outlying patches forming the tops of hills. It must
have been during the period when this denudation of the eastern
plains accompanied the gradual emergence of the continent, but acting
with very different results on the rocky sea-bottom and successive
ranges of iron-bound coast presented by the western slope, that
these immense deposits of shingle were formed and moulded into
terracesi.

* J have just heard that some Americans have discovered that there is gold
deposited by the Saskatchewan at the Rocky Mountain House. If so, it must
be washed out of the shingle-terraces along the eastern base of the mountains.—
Aug. 1, 1861. t Proc. Acad. Nat. Sci. 1858, p. 17.

t In many cases there is no doubt that the terrace-arrangement has been

406 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

But if this reasoning is to apply to the most ancient of those
accumulations, and so place them as more recent than the latest
Tertiary times, then there must have been a slight depression prior to
the steady and gradual elevation of the continent that has continued
ever since. Moreover, unless this depression was local and confined
to the mountain-region, how are we to account for the absence of
Post-tertiary formations over the high-lying Tertiaries of the plains
in sufficient quantity to have allowed time for the production of such
a gigantic formation of waterworn stones ?

On the other hand it is possible that their production may have
commenced in Tertiary times, so that they are almost coeval with
the great lignite-basin of the Missouri, which is an estuarine de-
posit. resting, according to Hayden, quite conformably on his Upper
Cretaceous beds.

He also describes his Titanotherium-bed, the lowest of the White
River Tertiary basin, which has yielded so many forms of chelonian
and mammalian remains, as likewise resting without a break of con-
formity on the Upper Cretaceous*. Thus if this latter suggestion
respecting the age of the most ancient of the terraces be correct,
they must have been formed in the straits and inlets of an archipe-
lago or rocky reef lying to the west of a flat Cretaceous continent,
in which were estuaries and lagoons choking with rank vegetation,
and large lakes, which gradually filled up, burying the remains of
the gigantic turtles and extinct forms of mammals.

In the Gulf of Georgia there are beds of conglomerate and coarse
sandstone overlying the Cretaceous strata to all appearance, and
which, I have thought, may perhaps correspond to the more ancient
of the mountain-terraces to which they bear a great mineral resem-
blance, excepting that those in the Gulf of Georgia have been much
disturbed, so that they are harder and their bedding is better marked.
The difference is, however, not greater than we should expect, if we
consider the one group to have been placidly raised to a great
altitude, while on the other the force has been expended in producing
plications and faults.

Drift of Pacific Coast—The glacial markings on the metamorphic
rocks of Vancouver Island are better displayed than I have elsewhere
seen them. Every surface near Victoria that is either naturally
exposed, or from which the soil has been removed, exhibits deep
parallel furrows, generally with a N.E. trend. They are also seen on
the main land at the entrance to Puget Sound quite as distinctly.
Erratics are distributed all along the Pacific coast, at least as far
south as latitude 46° N., where they occur, but not very plentifully,
near Vancouver and in the valley of the Willamette. They are
often of great size, and on Vancouver Island are composed of a grey

given to these deposits by the shore-line-action of lakes which formerly occupied
the i irregularities of the “surface of the country ; but we can hardly suppose that
the materi: al itself, consisting of smoothly worn fragments of the hardest rocks,
could have been entirely the “result of the feeble erosive agencies that such lakes
exercise.

* Proc. Acad. Nat. Sci. 1858, p. 19.

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 407

syenite, which Mr. Bauerman told me occurs in the Cascade Range.
Often in the woods to the south of Fraser River I saw solitary
boulders 6 or 8 feet high, resting apparently on the shingle-terraces
which here are only 100 to 200 feet above the sea. Certainly at
the Fourth Plain, five miles from Fort Vancouver, there are several
large blocks, though not of the above size, that do rest on the gravel-
terrace which skirts the valley of the Columbia River. On most of
the islands in the San Juan Archipelago, and along the coast of
Puget Sound, high sections of yellow sand and clay are exposed,
forming the sea-shore. The terraces are there further inland.
From this drift Mr. Bauerman procured casts of Cardium and
Saxicava.

As I never observed drift or boulders within the Cascade Range,
even in places elevated only 600 to 700 feet above the sea, but as
all the superficial deposits in the great trough between that range
and the Rocky Mountains are clearly formed from the rearranged
materials of the shingle-terraces along with tufas from the Cascade
Range, I conclude that the average lowest altitude of the Cascade
Range, which is somewhere about 4000 feet above the sea at the
present time, exceeded the depression of the continent during the
glacial epoch, and presented a barrier to the causes which transported
the erratics and scratched the rock-surfaces along the Pacific coast.
If the Cascade Range at that time formed a promontory enclosing a
gulf like the Gulf of California, it would exactly fulfil these condi-
tions.

TERTIARIES.

The existence of Tertiary* strata, ascertained to be so by their
organic remains, has only been proved at one point west from
the Cyprés Hills, where Mr. Sullivan obtained Ostrea Veleniana,
associated with a Modiola and a few other fossils, which Mr.
Etheridge, who has named all the Cretaceous and Tertiary fossils
brought home, has been unable to identify. The beds from which
these fossils were obtained consisted of friable sandstones with argil-
laceous and calcareous concretions, with massive and irregular bedding,
and often passing into incoherent pebble-conglomerate. Judging alone
from mineralogical resemblance, these beds were recognized over a
considerable area, but always forming high grounds in the neighbour-
hood of the Missouri Coteau, S.E. from the mouth of Belly River.

On the Souri River, seven miles north of the boundary-line, in
longitude 104°, was observed what is perhaps a portion of the
Missouri Tertiary lignite-basin. This locality, which is known to
the half-breeds as “ La Roche Percée,’’ is well up the eastern slope
of the Missouri Coteau, and within a degree of latitude of that river
itself, at a point where the existence of the lignite of Tertiary age
has been well ascertained.

The Souri River at this point flows through a valley with steep
sides, depressed 165 feet below the surface of the plain, which at this

* Using the term in its limited signification, as including Eocene, Miocene,
and Pliocene.

408 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

place is quite level, and strewn with an immense profusion of
boulders, being at the base of the Third great Prairie-level. The
sides of this valley are cut by numerous ravines, which only extend
a short way back into the prairie, and exhibit sections of the
following strata (see fig. 4) :—

Fig. 4.—La Roche Percée, in the Valley of the Sourt River: a section
of the Tertiary Ingnite Group.

a. Drift. b. Splintery limestone. e. Clay with lignite.

d. Coarse-grained sandstone. e. Concretionary sandstone.
Gx. Dritt waithyboulders: 15 sec seatota ce vation cee 4 to 7 feet.
Bo MNG=StONG diy: saptians yee crcl cunpmek aie uea Tanck ateleat ae 1 foot.

c. Incoherent sandstone, fine-grained, with hard con-
cretions impregnated with iron, which weather

GCONCeNbrICal yD. Svan cider ee seta oh a ns Ie 10 feet.
d Porous; calcareous simten: 2 amij-kaseiens isa eee 1 foot.
e Hard blue ironstone-shale, decomposing into deep

orange-coloured: splinters... /Sn)..0.. - anilenmuene 22 feet.
fe Saritty: limestones 5/24 ois asta MAly cs Se Bis Sabie

g Ash-coloured clay in thin indistinct layers, very soft,

with one bed of lignite 9 inches in thickness .. 8 ,,
h Hard blue limestone
t Same as g, but with thin seams of lignite 10, 8, and

6 inches. in thickness\s <3. Ss Sea a eee L5e ee
kee Grithy dimestone 0: 22 s\n bbe eee eee Zaks
l. Brightly coloured marls and shales, with selenite in

small: drarments):).2)ayhenveieleis eae et een 10)
m. Coarse-grained, incoherent sandstone more than.... 20 ,,

Excepting a few fragments of plant-impressions, like stems of
sedges, no fossils were obtained from these beds by which the age
could be identified. They may perhaps be passage-beds, representing
the highest strata of the Cretaceous era, overlain by the lignite-basin ;
as further south they are so disposed, and with very similar mineral
characters.

The lignite does not occur in well-defined beds, but graduates into
the shales on both surfaces. It is not visible until a light ashy deposit
is removed from the exposed edge of the bed, which has been formed
by the soft clay washing down from the strata above. The lignites
are of several different varieties, some having quite the texture of
compact cannel-coal of fine quality, some like the more glistening

1861. ] HECTOR—ROCKY MOUNTAINS, ETC, 409

bituminous coal, friable, and only to be obtained in small cubical
fragments, while some of it can hardly be distinguished from
charcoal, but all varieties have a deep purple-brown colour, which
is well seen when a portion is redueed to powder. A sample of this
lignite has been analysed in Dr. Percy’s laboratory, at the Museum
in Jermyn Street, by Mr. Charles Tookey, with the following
results :—

WALDON Tae. Soe eae te 56°50
Iv drO gen) wiry we ay tea ene 3°69
Oxyocnra ere eee 18-91
INGtrosene tec) 2h eee eee 0-80
Sulphur see eee May teat hOSOO
HAS Hata enee einen error ye antares 5°62
Water (hygroscopic) ........ 13-92

100-00

The sandstone which forms bed ¢ is composed of very fine pure
grains of quartz, hardly cohering ; but in the upper parts of the bed
there occur concretions impregnated with clay and iron, and of a
reddish hue, that are comparatively hard and decompose concre-
tionally. This irregular disintegratien gives rise to a curious
formation of the banks of the valley, which has rendered this lo-
eality an object of great superstition among the Indians. The lower
sandstone wears away from under the hard concretions, that assume
the form of compressed spheres, and sometimes long cylinders like
the boilers of a steam-engine, which are left supported on pillars of
the white sandstone. The gulleys which join the main valley are thus
filled with grotesque forms, sometimes exactly resembling the half-
buried remains of ruined edifices. The sandstone (m) at the base of
the section is also very incoherent, but is composed of larger grains
of quartz. The strata are not found in the same order and propor-
tion threughout the valley, but yet they always appear to be hori-
zontal, The marly shales (lettered /) have a considerable quantity
of selenite disseminated as small crystals. La Roche Percée is in
latitude 49° 6! N., and longitude 103° 54’ W.

This formation has, without doubt, been much more extensive,
and has overlain the Cretaceous beds as far north and east as the
great sandy waste where the track of the Expedition crossed the
Souri River in latitude 49° 30’ N., and longitude 100° 20’! W. At
that place the sand-hills rise 70 and 80 feet, so pure and so feebly
bound by the few plants that grow on their surface that they are
constantly windblown. Under these, and cut through by the River
Souri, was observed a lacustrine deposit in which one bed was com-
posed wholly of rolled fragments of lignite, overlain by sandy marls
and gravel, enclosing fragments of bones which Professor Huxley
refers to the Bison; and along with these were small land- and fresh-
water shells. This deposit has been found in one of the lakes, which
I referred to generally as of Quaternary age when describing the
superficial deposits of the prairies. The origin of this one has been

A410 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 10,

from the damming back of the water by the Blue Hills of the Souri,
which are composed of hard Cretaceous shales, and through which the
river of that name escapes to join the Assineboine by a narrow and
profound chasm which it has gradually cut through the horizontal
strata. The place where the sand-hills and the bed of lignite-pebbles
is found has been the north shore of the lake, which must have been
of very considerable extent.

The great valley of the South Saskatchewan where it is hemmed
in closely by the Grand Coteau at its elbow opens out above that
point, and at the junction of Red Deer River and Bow River in
longitude 109° 30’ W., latitude 51° N., the hills retire many miles
from the river, which, however, always preserves its immediate
banks of from 200 to 250 feet in height. The prairies are there
again covered with a waste of blown sand, which may perhaps have
had a similar origin from Tertiary or Upper Cretaceous beds, which
have been subjected to local denudation. The same iron-shot bands
containing the shells of land Molluscs and Bison bones were there
observed, but without any traces of the rolled fragments of lignite.

East from the elbow of the South Saskatchewan there is also a
tract of sand-hills with quite the same feature ; but there I observed
masses of sandstone zm situ, resembling the lowest beds at La Roche
Pereée. On the opposite site of the Qu’appelle Valley, within a few
miles from where I turned, the same sandstone occurs, and there Mr.
Hind found the characteristic fossils of the Upper Cretaceous group
(Rep. Assineboine and Sask. Exp.).

On the North Saskatchewan, forty miles above the elbow and
a little way above the Eagle Hills, on the left bank of the river, there
are cliffs of a very incoherent sandstone, rising 40 to 60 feet above
the water’s edge, and worn into caves, which often communicate with
the plain above. At the time I observed the sandstone, I took it
for a local variety in the drift. If, on the other hand, it belongs to
the Tertiary or the Upper Cretaceous group, it proves them to have
a very singular distribution, conforming in a great- measure to the
present river-valleys ; as on the opposite side of the river, at a little
distance back, the Middle Cretaceous group rises to the height of
several hundred feet.

Eight miles below the elbow of the same river, near Birch Gulley,
the banks rise abruptly on either side to the height of 210 feet, when
the level plain is reached at the point where the great erratic masses of
limestone rest on its surface. At the base of the bank from this
point, all the way down to Carlton, a distance of forty miles, springs
of water escape highly charged with iron and lime, which deposit a
light-yellow ochre. At the above locality the springs were seen to
issue from beds of sandstone and conglomerate, with travertine con-
taining dicotyledonous leaves.

The section is as follows :—

a. Banks of valley composed of Drift.

Coarse ferruginous sandvery moist, with beds of blue- and buff-
coloured clay, the whole having rounded boulders irregu-
larly dispersed.

ii i eh i

1861.] HECTOR—ROCKY MOUNTAINS, ETC. 411

b. 20 feet of coarse and fine sandstone impregnated with lime,
also gravel and shingle, and bed of travertine (c) with di-
cotyledonous leaves.

Ancient valley-deposit ?—or underlying the Drift ?

d. Present river-level with banks, 8 feet high, of silt and fine
sand, forming the “points” and densely wooded islands
in the channel.

I was unable to determine whether these beds have been formed,
like the silt-banks of the river, at a time when it was much larger
than at present, or whether they are beds cropping out from beneath
the drift. They are quite consolidated, but this may have resulted
from the calcareous nature of the matrix.

It will be seen that the observations I have made respecting the
distribution of the Tertiaries on the eastern plains are very disjointed
and unsatisfactory. As the Cretaceous strata overhanging the
Winnipeg group of lakes appear to dip to the west, again to rise to
the Coteau des Prairies, it is probable that the trough which they
thus formed was occupied by Tertiaries of the same age as those that
cover the Cretaceous strata on the Upper Missouri; but that, in the
immense denudation that has taken place, they have been unable to
withstand the erosion so well as the tough clays that underlie them,
which had therefore remained as a shoal further out to sea, while
along the shore the more yielding strata were being rapidly ground
down under the combined action of currents and stranded ice.

Although it is probable that Tertiary basins occur in the plains
further west, especially some of the groups that yield lignite, these
will be afterwards described along with the Cretaceous strata, as
there is an absence of data by which to discriminate them.

CRETACEOUS SYSTEM.

Nearly the whole of the great area of prairie country from the
eastern axis to the Rocky Mountains is occupied by Cretaceous
strata, which have attained an enormous development throughout
the central portion of the North American continent.

The classification of these strata, as they occur in the prairies to
the south, has been worked out during the last six years by Messrs.
Meek and Hayden with great success, and the results have been
published as memoirs in the ‘ Proceedings of the Academy of Natural
Sciences, Philadelphia.’ The Reports of the various Pacific Railway
exploring expeditions also give details and descriptions of the fossil
remains which have been found in this group.

Messrs. Meek and Hayden divide the Cretaceous System of the Upper
Missouri into five groups; but my observations were not sufficiently
extended to warrant my referring the different Saskatchewan strata
to these without much doubt, more especially as I had not the
benefit of their valuable reports, which were published while I
was engaged in the exploration. In the following vertical section I
have therefore adopted a different method of lettering, only indi-
eating the probable equivalents of their section. In the case, how-

412 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,
ever, of one group (EZ), Mr. Meck has identified the strata from
fossils submitted to him by Mr. Hind. The groups in my section
do not perhaps truly represent successive periods in time, but rather
indicate the different conditions that existed in the geographical
areas in which they were deposited.

Vertical section, in descending order, of the Cretaceous System, as
developed in British North America.

EF. Arenaceous clays and sandstones, ; Observed by Hind on South Saskat-

with Scaphites, Nautilus, Avicula, chewan below the Elbow.

and other marine Mollusca. Lower part of section at Ia Roche

No. 5 of Meek and Hayden. Percée ?
At the elbow of Battle River?

E. Indurated olive-coloured shales, with | Forms the high grounds cut through

bands and fissures filled with clay-
ironstone. Leda Hindi, Ostrea
lugubris, scales of Ctenoid Fishes,
Annelide-tubes, and Plant-remains.
Also observed by Hind, Natica, Ammo-
nites, &e.
No. 4 of Meek and Hayden.

D. Dark-purple and brown laminated
clays, with ironstone-septaria, and
sometimes crystals of selenite. Bacu-
lites, Inoceramus, Pholadomya, Car-
dium, Exogyra, Astarte, Cytherea,
Ammonites.

No. 3 of Meek and Hayden.

C. Sandstone overlying marly clays,
banded with thin seams of iron-
stone, thin beds of limestone, stiff
dark-blue clay, and arenaceous
shales. Ostrea cortex, O. vellicata,
O. anomieformis, Cytherea, My-
tilus, Cardium, Venus, Natica, &e.
Stems and roots of silicified trees.

B. Great lignite-group*; sandstones
coarse and friable, or argillaceous
and concretionary, indurated shales,
and soft limestones, ironstone-
nodules, beds of lignite 5 to 10 feet
thick: silicified wood, Taxites, and
sedge-like stems in the sandstones.

No. 1 of Meek and Hayden.
Includes the Wealden (?).

A. Green sandstone and conglomerate at
base of lignite-group at Nanaimo,
tufaceous sandstone-conglomerate,
much altered, and containing
Trigonia Emori, Cytherea Leo-
nensis, Arca (2 sp.), Psammobia,
Exogyra (2 sp.), Ostrea (2 sp.),
Rostellaria, Pecten, &e.

Jurassic ?

by Long Creek and the Souri River.
Also at the Forked Creeks near the
Assinebome.

Valley of Assineboine at Fort Ellice.

Elbow of South Saskatchewan, Eagle
Hills, and on North Saskatchewan
to Fort Pitt. On north slope of
Cyprés Mountain. In the Gulf of
Georgia, on Vancouver’s Island, at

Nanaimo River, Saltspring Island,.

and at Valdez Inlet, by McKay.

Battle River? Hand Hil!s, Red Deer

River.
(Not observed on west side of
Rocky Mountains.)

Red Deer River, North and South

Saskatchewan, Athabasca, and Pem-
bina Rivers, &c. Nanaimo, Van-
couver Island, Bellingham Bay,
Burrard’s Inlet, Gulf of Georgia,
&e. The position of this group is
not clearly made out to the east of
the Rocky Mountains, as the sections
at the first and second localities are,
so far as is known, contradictory.
The beds at Battle River, Edmonton,
and Lower Red Deer River may be
Upper Cretaceous or even Eocene.

Fossil Point, Departure Bay, North of

Nanaimo in Vancouver Island.

* It is possible that the lignite-bearing group B, which occurs in two lines

Eee

1861.] HECTOR—ROCKY MOUNTAINS, ETC. 413

Bituminous shales, resting on lime-| Described as occurring on the Mac-

stone and covered by friable sand- | kenzie River by Richardson.

stone. The shale takes fire and| Similar bituminous shales on the

burns spontaneously. North Saskatchewan and on the
The limestone contains fossils that are Athabasca where it cuts through to

Jurassic (?). outer range of the Rocky Mountains.
| From these shales perhaps come the | Containing Ostrea and Cardium.

two species of Ammonites described

by Hind. ]

[For comparison with the foregoing section I give three sections of the Creta-
ceous beds and the Tertiaries immediately overlying them, extracted from the
Reports of the Mexican Boundary-commission, vol. i. p. 126 e¢ passim, where
an able digest of their relations is given—prior, however, to the most recent of the
researches of Meek and Hayden.

First. Section of Eastern States. New Jersey.

VIII. Upper greensand beds (3rd).
VII. Coarse and fine beachsand.

“s ( VI. Middle greensand beds (2nd). :

= ‘ V. Quartzose sand, indurated and concretionary, with oxide of iron.
a § Exogyra costata, Ostrea larva, Belemnitella, Pecten.

= ao IV. Lower greensand beds (1st), marly clays.

Te Exogyra costata, Ostrea larva.

Soa Gryphea, Ostrea vesicularis.

Ee III. Dark-coloured clays, greensand in patches.

a Ammonites Delawarensis, A. placenta.

Pee iN A. Conradi, Baculites ovatus, and casts of Cardium.

Tn this position should be Nos. 2 and 3 of Meek & Hayden.

No. 1. of { II. Dark clays with fossil wood.
M. & H. | I. Fire- and potter’s clay, fossél leaves and wood.

Second. Section of Strata on Mexican Frontier.

Tertiaries of west coast. Miocene.
Tertiaries east of the mountains; sandstone, sands, and conglomerates
like those of the Mauvaises Terres in Nebrasca.
Calcareous beds with marine Kocene fossils underlying unconformably the
preceding strata.

Cretaceous.

1. Argillaceous beds. Hxogyra costata.

2. Calcareous beds, buff- and lead-coloured, with beds of white limestone.
Gryphea Pitcheri, Cardium multistriatum, Toxaster, Holectypus,
Ammonites Texanus, Hippurites, Nerinea, Caprina, &e.

3. Sandstones of various colours with beds of clay.

Carboniferous.
Third. Section from the Missouri westward.

Tertiary indurated clays, sandstones, conglomerate, and limestone,
with mammalian and chelonian remains, and fresh-water shells.

Y,
Res & 5. Arenaceous clays, argillo-calcareous sandstones. _80 feet.
oe Rares 4, Plastic clays, concretionary calcareous sandstone.
pace the Newey ‘ 250 to 300 feet.
Jersey Section. |
C. & D. of

Nicollet. } this is the principal fossil-bearing bed of the Upper Missouri.

separated by a belt of clays like C, may include deposits of two different ages—
the one Upper Cretaceous or Hocene, like the beds at La Roche Percée, and the
other Cretaceous, in the position assigned to it in the section.

VOU. XVII.—PART I. 2F

Aj 4 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [ Apr. 10,

MOS Book 3. Calcareous marl, Ostrea congesta, Inoceramus problematicus,

Nicollet | scalesof Fishes . . . . . . . . 100 to 150 feet.
‘ 2. Clay with few fossils . ah

Nos. I. & IT. of

New Jersey.

“The change from III. to IV. is always well marked.

“* Inoceramus problematicus, which is the same as J. fragilis, is the characteristic
fossil of Nos. If. and II1., and with Ostrea congesta ranges to Mexico.

‘These latter groups everywhere rest on the sandstone and clay beds (No. I.),
which are the ‘Jurassic’ of M. Marcou.

“With the exception of two species, the Cretaceous fossils of the Mexican
frontier are distinct from those of the New Jersey section, and nearly equally so
from those of Nebrasca; whereas the latter or Nebrasca section, extending from
the Missouri westwards, has many fossils in common with those of New Jersey
and Alabama. It is therefore probable that the Mexican beds represent a
different epoch in the Cretaceous series from those of the east and north-west.
However, from the Mexican frontier no sections were obtained to show whether

one or more groups were represented.”—Rep. Mex. Boundary-commission,
vol. i. p. 126.]

: 80 feet.
hi. Sandstone and clay with fossil wood. . . . . 90 feet.

Group F.—In speaking of the Tertiaries, I have mentioned the
only places where it is probable that the route of the Expedition
touched on the strata of this group—viz. at the height of land of the
Qu’appelle River and at La Roche Percée, where the lower sandstones
may perhaps be of this age.

Group E.—By reference to the map, it will be seen that the first
point where the route of the Expedition passed over Cretaceous strata,
was after gaining the great plain of which Pembina Mount forms the
eastern limit, at Long River, latitude 49° 8’ N., longitude 95° 35’ W..,
which is a tributary of Pembina River, flowing northwards. This
stream flows through a deep valley in the high plateau stretching
back from Pembina Mount, and in its gulleys are exposed sections
of group B. It is a compact shale of light greenish-drab colour, not
occurring in continuous layers, but as fragments with irregular
conchoidal surfaces, which have been produced by the desiccation of
what were originally thin layers of clay. Sometimes it has more of
a slaty character. Among these beds are hard bands and nodular
masses of dark-brown clay-ironstone, and perpendicular fissures are
common, which are filled up with splintery iron-shale. Also small
coloured tubes traverse the strata perpendicularly in large numbers.

The same strata were observed at Forked Creek, where a deep
eulley joins the valley of the Assineboine in latitude 50° 6’ N., and
longitude 101° 18' W., and these two places are both on a line of
high hilly ground, which stretches in a north-west direction, no
doubt marking the outcrop of the shales. At Long River they dip
gently to the south, and are covered by 6 feet of pure white sand,
very incoherent ; and over this lies the Drift, consisting of light-grey
ealeareous earth. At Forked Creek they seemed to be strictly hori-
zontal, and were covered by a local drift derived from the subjacent
beds. Mr. Hind, who also saw the beds at Forked Creek and other
localities, submitted the fossils which he obtained to Messrs. Meek and
Hayden ; and they have referred them to their second highest group.
He gives the following list as named by them* :—

* Rep. Sask. Exploring Expedition, p. 180.

ee

1361. | HECTOR—-ROCKY MOUNTAINS, PIC. 415

Anomia Flemingii. Natica obliquata.
Tnoceramus Cedarensis. Avellana concinna.
Leda Hindi. Ammonites (sp. indet.).

Of those from my collection has been determined the Leda Hind: ;
and, in addition, Ostrea lugubris, scales of Ctenoid Fishes, Annelide-
tubes and Plant-remains were also found. Traces of these beds were
observed to the south of the Qu’appelle River, and also on the North
Saskatchewan on the left bank, a considerable distance above the
Eagle Hills. Mr. Hind also observed them to form part of the high
escarpment of the Duck and Riding Mountains which overhang the
lakes, reaching an altitude of 1000 feet; and it was at 500 feet from
the summit that he detected these strata.

The group has not been distinguished from the next on the
map which accompanies this paper; but, from the more resisting
texture of these shales, it is probable that they occupy a larger area
of the lower plains that have been subjected to such great denudation
than any other group of strata.

Group D.—At Fort Ellice the banks of the Assineboine are 240
feet high, and in general their structure is obscured by vegetation,
but at one point a recent slide displayed a partial section of the bank.
The upper part consisted of the comminuted fragments of the last-
described shale, along with beds of pure sand, and also the more com-
mon yellow drift. Close to the water’s edge, masses of strataof tenacious
calcareous clay were exposed, of a dark-purple colour, but presenting
a weathered surface decomposing into a ferruginous earth. Along
with these strata were two beds of soft clay-ironstone about 4 feet.
apart ; the lower one half a foot thick and rather compact, the upper
one concretionary, forming thick nodulated masses, the surfaces of
which show the cone-in-cone structure. At this place only a few
fragments of the nacreous shell of Baculites were found, but suffi-
cient, along with the mineral resemblance, to identify these beds with
group D in the vertical section. At the elbow of the South Saskat-
chewan, where that river cuts through the great prairie-céteau, the
boulder-drift is seen to rest on strata of purple clay (fig. 1, p. 395),
with nodular masses of ironstone, having vems and cavities filled
with calc-spar. These Septaria are in great numbers, and, when
broken, are found to include fragments of the following fossils :—

Baculites compressus. Cardium.
Tnoceramus (/. Crepsii of Roemer Exogyra.

and Conrad). Astarte Texana.
Pholadomya occidentalis (Morton). Cytherea.

The outcrop of these Septaria-clays has a clear relation to the
great prairie-ridge which is cut through by the South Saskatchewan
at this point, and continued to the north-west by the Eagle and other
hills to near Fort Pitt, where it hems in the North Saskatchewan in
like manner, the banks having an altitude of 500 feet, and also dis-
playing sections of the strata with the same fossils. At the base of
the Eagle Hills, and wherever they prevail, they form lofty and
ruinous banks, the strata breaking away in great slices, which slide
forward successively. I have counted as many as thirteen such slides

22

416 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

on the bank of the river; the oldest, though now close to the water-
level, still bearing part of the original prairie-surface, with the same
turf that once grew 200 or 300 feet above its present position. The
result of this is, that it is seldom that anything can be learnt of the
strata which form the full thickness of the river-banks, the more
superficial beds being repeated again and again in each slip, so as to
give a very exaggerated idea of their development. Above the elbow
of the South Saskatchewan the strata are very dark, and contain a
large quantity of selenite in radiating crystals. Portions of those
soft strata have been formed at this place, by the action of the weather
and of the river on their base, into lofty conical mounds, which
present a most extraordinary appearance. As no grass has time to
grow on them from the constant attrition of their surface, they are
perfectly black, and their outline is broken into terraces by the
successive lines of ironstone-concretions, which from their hardness
retain the soft strata underneath them. At the base of the Cyprés
Mountains, where these hills begin to rise from the plains that lie
between them and the South Saskatchewan, the sides of the coulées
are formed of the same Septaria-clays, with fragments of Jnocerami,
and presenting the usual rugged features. This locality would be
very favourable for the study of the whole Cretaceous group and
the overlying Tertiaries which form the summit of the high lands of
the Missouri Coteau, were it not so dangerous on account of the
different hostile Indians that move about in strong parties through
it. The Expedition only spent a very few days at this interesting
place, as it was here that we broke up into parties to explore the
Rocky Mountains in 1859. From the few observations I was able
to make however, I have been induced to carry the line of these
strata from the elbow of the south branch along the céteau to the
Cyprés Mountains, besides their outcrop to the north-west, along
the line of the Eagle Hills to Fort Pitt. In the prairies this and
the other groups of the Cretaceous System preserve an unaltered con-
dition, and rarely present other than a most gentle dip; but close to
the Rocky Mountains, and also within the plications of the older
rocks forming that chain, altered shales, highly charged with iron
and resting on sandstones, were observed, which at the time I was
inclined to consider to be these Septaria-clays, as the concretions had
a very great resemblance to those of this group.

Similar beds with Inocerami were also observed at Nanaimo on
Vaneouver Island, but I shall describe the whole strata at that
place together, and for the present confine myself to the development
of the Cretaceous System in the Eastern Prairies.

Group C.—A very large proportion of the higher plains to the
west of the Eagle Hill Coteau is occupied by the fourth great group
of the Cretaceous strata. It is met with forming the banks of the
lower part of Red Deer River, near where the Expedition crossed it
during the last summer’s explorations. From that part it rises to
the westward, until, at the Hand Hills, the sandstone which forms
its upper member has preserved it as outliers, having abrupt escarp-
ments to the west. By its marked lithological character it was also

1861. ] HECTOR—-ROCKY MOUNTAINS, ETC. 417

recognized on Bow River to the south for a considerable distance
above the mouth of Belly Biver, and also yet further to the south-
west, forming the high broken grounds over which I passed on my
journey from the Cyprés Mountains to the Rocky Mountains in
August 1859, It was also met with at the elbow of Battle River,
and above Fort Pitt, on the North Saskatchewan, where it seems to
form the banks of that river for a considerable distance, but is
wanting above the Snake Portage, until it reappears again at the
Pyramids about 100 miles above Fort Edmonton. Between these
points it probably forms the high grounds back from the river, such
as the Beaver Hills, Bears’ Hill, and the hills round St. Ann’s to
the west and north of Edmonton. I offer this sketch, however, of its
distribution more as a surmise founded on the physical features of
the country, than from actual observations of its relations at these
various points,

Excepting very obscurely below the Snake Portage on the North
Saskatchewan, I cannot say that I anywhere observed the relation
of this group to the Baculite-clays of the preceding division. I
descended that river on the ice, travelling with dogs, in March 1858,
and as the late season compelled me to travel a great deal in the
night I missed many points of interest. Its relations to the strata
below it were apparently shown on Red Deer River.

At this place the group is found to form the broken country round
the base of the escarpment of the Hand Hills, which probably in
their full altitude include several of the members of the Cretaceous
System, and therefore merit a more minute description.

These hills form a high mass of table-land a few miles back from
Red Deer River, presenting an abrupt escarpment to every quarter
but the east, in which direction they slope off gently with the dip of
the strata.

Our encampment on June 25th, 1859, was in one of the deep
ravines on its western face, 375 feet above the plains below, and 160
feet below the level of the plateau above.

In the upper part of the escarpment facing the 8.W., grey coarse
sandstones were exposed, which had a considerable dip to the N.E.
The bedding of these was hard and distinct, and they were seen to
rest upon soft incoherent sandstone underlain by light sandy clays and
blue-clay shale (see section, fig. 5). In the clays are enclosed angular
masses of black iron-shot sandstone, and also pebbles of quartz and
granite. No evidence of the exact position of these strata was ob-
tained ; but, although they were somewhat disturbed, I saw no reason
to doubt that they are a superior member of the Cretaceous series
overlying the beds next to be mentioned, which are of the group
C. Fig. 5 (p. 418) gives a sketch of the strata of the hills from the
valley of Red Deer River northwards ; and it will be seen that there
is an interval of several hundred feet between the sandstones and
clays and the banded clays of group C, the nature of which was
not ascertained. These banded clays, which occupy a narrow tract
of country round the Hand Hills, give rise to large white mud-
swamps, which we found at the season of our visit to be nearly dry,

418 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

and presenting a very rough surface from the floundering of the
large herds of buffalos in the tough
plastic clay bottom as they had been
eagerly striving for the last trace of
water. These clay beds, which con-
tain a large proportion of calcareous
matter and are often “ bandea” by
thin seams of soft ironstone, have a
white chalky aspect, and are so easily
acted on by the weather that what
were originally gulleys soon expand
into wide flats bounded by conical
hills, with bright surfaces marked
regularly at every few inches by the
parallel streaks of ironstone, which
are often only half an inch thick.
From these swampy flats, that serve
as reservoirs for the water which de-
scends from the hills in spring, the
streams have worn deep ravines which
join the valley of Red Deer River. At
the commencement of one of these,
or near the base of the group C, the
«panded clays” were seen to rest on
red iron-clay shales in thin beds,
underneath which is a bed of rotten
limestone of a buff colour, which again
rests on a bed of shell-conglomerate,
principally composed of fragments of
Ostrea cortex aggregated into a solid
rock with many complete specimens of
the same shell. Mr. Etheridge has
identified this shell, which is a spe-
cies described by Conrad in the Mex-
ican Boundary Commission Reports
(p. 157). Together with Ostrea mul-
tilirata it was found at Dry Creek,
Mexico; and, in describing them,
Conrad says that he knows no species
like them in the Cretaceous System,
and that probably they belong to

Hand Hills.

e. Ostrea cortex and Cytherea Texana.

h, Sandstones and dark clays.

d, Paludina, &e.

4 miles.

ec. Silicified mood:
g. Banded marlites.

b. Brown coal.

Fig. 5.—Section from the Red Deer River to the Hand H ills: the Middle Cretaceous and Lignite Groups.

strata of still earlier date. However, aS
at another locality, near the Hand Hills, : = s
T again found Ostrea cortex, and along 28
with it O. vellicata and Cytherea = 3
Tecana; and these are undoubted ay
Cretaceous shells of Mexico. From nee

between El Passo and Fontera, which

"3393 009
seem to be places within a few miles of each other, the following

list of fossils is quoted in the Mexican Boundary Report—0O. velli-

1861. ] HECTOR—ROCKY MOUNTAINS, ELC. 4i9

cata, Cytherea Texana, Kxvogyra (2 sp.), Lrigonia Hmort, Arca, and
Nodosaria,—thus including both fossils found in the neighbourhood
of the lignite on Red Deer River, and also some that were found along
with that of Vancouver Island.

On Battle River, in latitude 52° 17’, the banded clays were also
observed with the same features and with the same fossils. From
that river to Red Deer River they appear to form the surface of the
country, as every shallow ravine shows slides of the white chalky beds,
and the white mud-swamps are very common. At the “elbow” of
Battle River, the strata have a slight easterly dip; and in the upper
part of the bank were obtained in a concretionary sandstone Avicula,
Cardium, Cytherea, and Baculites compressus.

A little higher up the river, and towards the base of the bank,
Ostrea cortex was found, as on Red Deer River. For fifteen miles above
this point the valley is cut through these strata ; and then the banded
clays are seen to form the higher portion of the banks, still with
rolled fragments of Ostrea at their base in some places, and resting
on strata containing silicified wood, which form the lower part of the
bank, while in the bottom of the valley the true lignite appears.

Group B.—In my next and lowest group I have (with great
hesitation) classed the large deposits of coal or lignite, of the Prairie-
country, that are sufficiently compact to be of value as fuel, but
which have hitherto been generally classed as of Tertiary age.

However in all the sections which have been given of the Creta-
ceous System in the United States, it will be observed that the lowest
beds are always described as sandstones containing fragments of fossil
wood. Further, Dr. Hayden has pointed out that, at the base of his
Lowest Cretaceous group fresh-water beds occur, in which the shells
are more nearly allied to Tertiary forms, and that the vertebrate re-
mains, of which only a few bones have been obtained, are considered by
Dr. Leidy to belong to an equivalent of the Wealden period in Europe.
In the same horizon has also been found angiospermous leaves, such
as Quercus, Salix, &e. At the same time he remarks that the fossils
from the Judith River beds of the supposed Wealden age cannot be
distinguished in many instances from those of the great lignite-basin,
which he knows to be Tertiary beyond doubt, mentioning as instances
an Ostrea and a Trionya that were considered common to the two
formations. It may therefore be justly concluded that this question
is one of great nicety and doubt, which will only be slowly cleared
up as those vast territories become explored. Nevertheless, we are
by these observations prepared to consider as possible at least the
existence of a coal-bearing formation at the base of the Cretaceous
System, even though developed to an extent not hitherto recognized*,
In his description of the lignite-formation on the Mackenzie River,

* Since writing the above, I have seen a paper by Dr. Hayden, published in
1857, and before the only other memoir of his that I had access to, in which he
suggests that his Lowest Cretaceous group may be only an extension of the lig-
nite-group which extends from the Arctic Ocean, but which, ‘ike that group at
Judith, may be mixed up with Tertiary strata, also containing lignite—Proce.
Acad. Nat. Sci. May, 1857, p. 116.

42() PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

Sir John Richardson refers to strata of a similar nature as occurring
at Edmonton on the North Saskatchewan; and, on first arriving at
that place in January 1858, I had no difficulty in identifying the
beds there with those which he describes. I got not only the same
yew-like leaf ( 7awites) that he figures as characterizing the shales, but
also the same general succession of strata, excepting only the beds of
shingle and gravel, which he describes in his sections of the Mackenzie
River. Before leaving England, Colonel Lefroy furnished me with
the following extracts from his notes on Peace River, a point midway
between the Mackenzie and Fort Edmonton, which are suflicient to
show that the strata are probably continuous throughout this area.
He observes that ‘‘ at the ramparts on Peace River is a vertical cliff
of sandstone with broken stratification towards the top,” and that “ at
Dunyegan the river is depressed 600 feet below the general level, and
great quantities of crystals of sulphate of lime were collected in the
upper strata, while actual coal occurs in the seams about ten miles
above the fort on one of the small tributaries.”” The lgnite-for-
mation has also been remarked on Smoking River, a tributary of
Peace River; and I have traced it on the Athabasca and McLeod
Rivers, and on Pembina River, all to the north of Edmonton; thus
proving the range of this formation over a slope rising from 500 to
2300 feet above the sea, and yet preserving on the whole the same
characters, and showing no evidence of recent local disturbance
beyond the gentle uplift which has effected this inclination.

I shall now describe this formation as it was observed in different
parts of the country explored, commencing with the North Saskatche-
wan. The lowest point on that river where the coal was actually
observed, was about two miles below Fort Edmonton, where a thick
bed of it was seen dipping gently out of sight below the water-level
tothe N.E. I have reason to believe, however, that other beds of it
occur further down the river for a distance of 50 or 60 miles.

At Fort Edmonton the flanks of the river-valley are from 190 to
250 feet high, and at most places densely wooded. Seven to ten miles
back from this valley, on either side, a line of high ground rises from
200 to 300 feet above a willow-covered plain, and consists, as far
as I could learn, of the white marly clays of the group D; but the
country in this neighbourhood is much obscured by superficial deposits
and by small copse-wood. The river-valley has a wide flat bottom
through which the river winds in a channel 40 to 60 feet deep, and
wherever this present channel sweeps close under the higher valley-
banks, sections are displayed, disclosing horizontal strata of arena-
ceous clays, sometimes passing into clay-sandstone with spherical con-
cretions, but at others into clay-shales. Many of these beds are highly
charged with nodules of clay-ironstone, which are filled with commi-
nuted fragments of vegetable matter. The coal occurs in the clay
strata, and varies greatly in purity. It is used in the forge at the fort,
and is found to answer very well, excepting that it ‘“‘ burns” the iron
more than ordinary coal. It ignites with difficulty, but keeps alight
for a very long time, and, if left to itself without a draught, smoul-
ders away into an abundant orange-coloured ash, It contains a quan-

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 421

tity of water in its composition, as, although generally compact, like
fine bituminous coal, when first excavated, it soon splits up into frag-
ments which have dull earthy surfaces. There is a great difference in
the quality of this lignite or coal, according to the bed from which it has
been procured, and also the distance from the outcrop to which the
seam has been worked. ‘There are no sinkings of any sort into any
of the seams, the manner of procuring the small supply which is
required for use at the fort being for the blacksmith to go down to
the river-bank with a pick, and procure a few basketfuls where he
can most easily get access to the material.

The fort stands about 100 feet above the water-level, and below
it in the bank there are two seams of 18 inches each, but on the
opposite side of the river, at a little distance below, there are several
seams exposed, the principal of which, close to the water’s edge, is
6 feet in thickness ; and there is one a little way higher where it is
4 feet, with others less pure (see fig. 6).

Fig. 6.—Section of the Right Bank of the Saskatchewan River
near Fort Edmonton.
A

SSS cen cocereeonencorestasieco

Superficial sand and gravel.

Grey sandy clay.
Lignite, 1 foot.

Shale.
Lignite, 2 feet.

60 feet.

Clay-sandstone.

Lignite, very pure, 3 fect.

Concretionary greensand.

Lignite, pure and compact, 6
feet thick, with an interca-
lated band of soap-clay, 6
inches thick.

In the middle of the 6-foot seam there occurs a layer, 5 to 8 inches
thick, of magnesian steatitic clay, which works up into a lather like
soap, and is used by the women at the fort for washing blankets.

A sample from the 6-foot seam has been analysed, at the same
time with the Lignite from La Roche Percée (see p. 409): Mr.
Tookey’s results are as follows :—

(CEnA IONS sheers gla Seat hel tira ey Geel eon SEN 50°60
A Tay ROR EM Net roiiatnecesle vaedursier ess S)chaes: 5 3°24
INSIRO COM Nate Wc uae eigen sine (sa eae. 0:90
Oey SO ae Perinat set acer! wine GluarS 3 14-41
Suilip ueeeeea ieee enone rc cent a 0-42
PASTING peer te Bie Macey ha rse a cok wit cP 15:93
Wiater (nyeroscopic)m met. alesis 14:50

100.00

“ The colour of the ash in each case was buff. When heated in a close

422 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

vessel, neither of the lignites yielded a coherent coke, the residue
retaining as nearly as possible the shape and bulk of the original
particles. The gas which was expelled during the process possessed
but feeble illuminating powers. Both samples contain a large per-
centage of water that can be expelled with a temperature of 100° C.
This appears to be a characteristic feature in the composition of
lignites.”

The gravel- and shingle-deposits are seen to rest on the cut edges
of the coal-bearing beds, and are therefore of more recent date.
They contain fragments of the nodules derived from the underlying
strata, along with pebbles of quartz and other rocks, that must have
been derived from elsewhere. Also large fragments of silicified wood
are found in the subsoil at Edmonton, the same as that found in
the upper part of the lignite-group on Red Deer River, as will be
described.

At the bend of the river below the fort, and on the same side,
the bank looks as if broken tiles had been strewn over it. This
arises from the coal having at one time been completely burnt out,
only being represented now by a thin layer of ash, while from the
baked clays above and below the red tile-like material has been
derived. Amongst these fragments I obtained impressions of the
same Yew-hke leaf that Sir John Richardson found in the beds at the
Mackenzie River under similar circumstances, but along with dico-
tyledonous leaves, of which I however found no trace.

For ninety miles up to the North Saskatchewan, above Fort Edmon-
ton, the grey arenaceous clays prevail, forming the banks of the river,
which are high and precipitous, the valley for that distance making a
succession of abrupt bends after every few miles of a straight course,
its main direction being to the north.

The secondary banks are also gradually lost, until at length, from
the valley narrowing, the river occupies its full width. Above this
point, however, the valley suddenly widens and preserves on the
whole a straight course from the west, independent of the windings of
the river itself, which has a very tortuous course between secondary
banks, crossing from side to side of the great valley round heavily
timbered flats. Where the river sweeps under the high banks, sections
about 200 feet high are exposed of white variegated marls, which are
cut in the most regular manner by gulleys into pyramids, with a most
artificial appearance as seen from the river, their bright chalky sur-
faces being thrown into strong relief by the dark-green pines that
clothe the ravines. These marls have much the look of those of
group C.

Fifteen miles below the mouth of Brazeaus River, which is a large
tributary to the North Saskatchewan from the west, we again meet
with the lignite-bearing arenaceous strata, and from this point they
were traced uninterruptedly to the base ofthe mountains. The forma-
tion now presents very different characters from those at Edmonton,
having more the appearance of a shore-deposit. The mineral compo-
sition is very varied, and large deposits of sandstone occur, which is
fine- or coarse-grained, but never makes any approach to a conglome-

1861.]

KY MOUNTAINS, ELC. 423

rate. At the Rocky Mountain House, in latitude 52° 21’ N., longi-
tude 115° 10’ W., where Lhad the best opportunity of examining this
formation, I divided it into three groups, judging from the mineral
composition alone ; as they were found to pass from one to the other
without superposition, just as we might expect to find in a shallow
lagoon-deposit.

Ist. Coarse-grained sandstone, composed of angular grains of
quartz cemented by calcareous matter, present in small quantity.
This sandstone forms bold perpendicular cliffs, often 150 feet in height,
and hemming in the river on both sides. It resembles the descrip-
tions given of the sandstone of the “‘ ramparts” on the Mackenzie and
Peace Rivers; and indeed on all the rivers this formation may be
traced by this marked feature as far south as the Missouri at least, as
a drawing of the falls on that river (given in Pac. Rail. Rep.) exactly
resembles these sandstone cliffs.

The 2nd group consists of beds of green argillaceous sandstone,
which, as it weathers easily, always gives rise to sloping banks,
from which protrude concretionary masses. These beds are gene-
rally horizontal, but sometimes present a rapid dip towards the
edges of basins in the last group in which they seem to have been
deposited. They are, however, often overlain by the hard-bedded
sandstone.

The 3rd group more resembles in its mineral characters than the
other two the beds at Hdmonton, consisting of alternations of clay-
shale and argillaceous sandstone in irregular beds, and including
deposits of coal or ignite. The shales, which are often very hard and
compact, contain fragments of the Yew-like frond, and also stems of
plants like sedges.

Fig. 7 (p. 424) is an attempt to combine the different sections that
were observed at the Mountain Fort. The irregularity in the mineral
composition is well shown about five miles above that place, where in a
very short distance beds of clay and soft green sandstone are suddenly
replaced by cliffs of grey and yellow sandstone with heavy bedding*.

* The features of the strata at the Mountain House are very similar to the
description given of the Lower Cretaceous groups at Seargent’s Bluff on the Mis-
souri by Meek and Hayden, where the following section is described :—

“‘1, Dark-coloured clay with sandstone seams . . . . . 6 feet.

2. Light-yellow clay passing into grey sandstone OMe;
3. Dark clay with fragments of carbonized wood eta
4. Grey indurated clay or marl with wood hs
5. Dark seam like No. 3. 8 inches.
6. Clay like No. 4. 3 feet.
7. Grey sandstone (carbonized wood) . Dinas
8. Very dark-grey clay, sometimes black, with or ganic matter
in the lower part, and crystals of selenite! NO. 3
9. Grey clay, carbonized wood and hard concretions . S00
10. Grey sandstone with wood . PAN a

tl. Grey clay, with wedge- shaped masses of hard bituminous
lignite or coal and round lumps of sulphuret of iron,
to the river-level” . slipuisiee fel nosn ae mieecaea tc Levan
It is mentioned that the beds thin out in many directions, and that some in-
crease to a great thickness in a few hundred yards.

(Mexican Boundary Rep. vol. i. p. 136.)

424 PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

As developed at the Mountain House, this formation, whatever

its exact age, may be described as con-
sisting of sand and clay in varying pro-
portions—ereat ridges of pure sand-
stone, including basins in which have
been deposited clays and clay-sand-
stones charged with coal and ironstone
in large quantities.

On the Athabasca River, the valley
from Fort Assineboine in latitude
54° 50! up to the outer range of the
mountains at Deadman’s Rapid, cuts
through argillaceous sandstones, with
beds of clay and coal of the same kind
as those at the Mountain House. The
sandstones are in much greater propor-
tion however, and the lignite-beds are
more rarely seen, than in the sections
along the North Saskatchewan. At
Deadman’s Rapid these strata are suc-
ceeded by grits and clay-shales in
regular beds, undisturbed at first, but,
on approaching the mountains, found
to be implicated in the late upheavals.

On Red Deer River the lignite-
formation was observed at various
points, the lowest being at the Hand
Hills, which have already been alluded
to in speaking of the “ banded clays.”
By again referring to fig. 5 (p. 418), it
will be seen that a flat plam extends
back from the summit of the river-
valley towards the base of the hills
where the white mud-swamps are situ-
ated, but which is cut up by great
ravines, Which gradually deepen as
they approach the river. The river-
valley itself is half a mile wide, and
270 feet deep.

At the commencement of one of the
ravines, about three miles back from
the river, were found the fossils before
mentioned (Ostrea cortex); and in
another, at only a quarter of a mile
back from the river-valley, that fossil
was again found in the highest part of
the bank, along with Cytherea Texana,

f an ancient valley.

reensand.

6. Fine-grained concretionary g

s. Shingle and gravel forming terraces o

6 miles.

ds and the terraced arrangement of the Superficial Deposits.

the Saskatchewan River, at Rocky Mountain House, combined in order to show the
ements of carbonized wood.

variation in the be

Fig. 7.—Sections along

qd. Coarse-grained sandstone ; with fra
ec. Shales with lignite and ironstone.

showing that these beds must form the surface of the level flat.
the mouth of the same ravine (Shell Creek), the following sections
were observed in the bank of the valley of Red Deer River, the beds

being to all appearance horizontal :—

1861.] HECTOR—ROCKY MOUNTAINS, ETC. 425

a. Buff, unstratified, earthy clay.—12 fect.

6. Ash-grey and cream-coloured sandy clays in bands with thin
seams of clay-ironstone and carbonaceous layers (‘‘ Band-
ed clays’).

Throughout this bed are angular pebbles of ironstone which
look like fragments of septaria.—30 feet.

c. Seam of pure lignite (“ cuboidal lignite ”)—3 feet.

d. “Banded clays” very sandy in some places. In other places
the coal has been burnt out and the heat has converted the
upper beds of this group into material like broken tiles,
which lie scattered over the banks. Probably the ochre-
beds observed in some parts of the banks are the layers of
ash which represent the lignite-bed when consumed.

f. Brown coal. This bed is about 18 inches thick, and in thin
leaves, with a paper-like texture ; on it rests—

e. | foot of silicified wood, composed of stems and trunks, and
roots of large trees. In the bed these are of a deep
brown-black colour, but the fragments which lie scat-
tered about weather to a light-cream colour on the sur-
face. One silicified root measured 18 inches in diameter.

g. Sandy clays partially banded, varying from grey to light-cream
colour. Crystals of selenite are very common, but no large
masses were observed. This group has a very chalky
look from a distance. It is probably 100 feet thick, but
the base of the section was not observed.

Although these beds are very variable, passing horizontally into
different varieties of shales, banded clays, and sandstones, still there
seemed to be a definite inclination to the N.E., so that in ascending
the river deeper beds were exposed.

A few miles above Shell Creek the lower part of the banks are to
a great extent composed of a bed highly charged with ironstone
nodules, which have very irregular shapes, unlike the nodules in the
other parts of the strata. The profusion of these strewn on the
slopes of the valley reminded me of the heaps of roasted ironstone
scattered in the neighbourhood of iron-furnaces. A little way
further on, where a creek joins the valley, thick beds of coal
appear at the base of the section. The lowest bed is 4 to 5 feet
thick, and very compact and pure. It is included in the same gritty
sandy clay that everywhere forms the matrix of the coal.

The iron-shales immediately overlie these beds, and these are again
overlain by the “banded clays” that form the base of the section
lower down. By following up Coal Creek for a few hundred yards
to where the banks attained a height of 250 feet above the burnt
lignite-seam, I found in a hard sandy limestone-bed the following
fossils :—

Ostrea anomizformis. Crassatella.

Mytilus (2 species). Venus.

Cardium multistriatum. Rostellaria.
Paludina.

No break was observed in the beds, and the succession of the strata

\

426 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

from the lignite upwards was such as might be expected in a gradual
passage from freshwater to marine deposits. I did not, however,
remark the layer of silicified wood or brown coal that I expected to
occur above the “ banded clays” that overlie the lignite.

On Battle River similar beds were observed in lat. 52° 28’ N.
long. 111° 29’ W., having the same order. The high part of the
section was composed of the “‘banded clays” along with concretionary
masses of sandy limestone, containing Ostrea, Avicula, and other
shells. Over the “banded clays”? is the layer of silicified wood,
while at the base of the section and under the water of the river
the beds of lignite crop out.

For sixty miles above the Hand Hills I had no opportunity of ex-
aminine the banks of Red Deer River, but at the mouth of Bull
Creek the strata were found to present much the same appearance
as at that place; the higher banks consisting of the “ banded
clays,” while along the river are exposed the beds of lignite overlain
by the silicified wood. Beneath the lignite, and what must be the
lowest bed of the section at this place, occurs a hard grey sandstone
with large concretions, that contain a slight admixture of lime, and
in these I obtained several leaves of deciduous dicotyledonous trees.
The exact spot where these were obtained is just below the mouth of
Deadman’s Creek. A little above this place the coal forms beds
of great thickness, one group of seams measuring 20 feet in thickness,
of which 12 feet consist of pure compact coal, and the remainder
of carbonaceous clays. At one point the seam was on fire, the bed
exposed in a cliff of about 300 yards in length being at many places
in a dull glow, the constant sliding of the bank continuing to supply
a fresh surface to the atmosphere. For miles around the air is loaded
by a heavy sulphurous and limey smeil, and the Indians say that for
as long as they can remember the fire at this place has never been
extinguished summer or winter. For ten miles above this place the
coal-beds were traced as we ascended Red Deer River. They are
then succeeded by cliffs of sandstone apparently formed by beds over-
lying the coal-group, but the dip is very slight. The Nick Hulls
where this sandstone forms a high ridge run to the north-west,
and above this point the banks of the river are composed of finely
laminated marly clays, often containing concretionary masses of lime-
stone filled with freshwater shells, such as Paludina, Planorbis, &c.

Fig. 8.—Seetion on the Saskatchewan River, 20 miles above

Rocky Mountain House.

Se ae |

1861. | HECTOR—-ROCKY MOUNTAINS, ETC. 427

seem to occupy a great basin, through which the river flows from
above the forks of Medicine River. Traces of a similar deposit of much
more recent date than the lignite-group on which it rests, were no-
ticed on the Athabasca River and also on the North Saskatchewan,
as shown in fig. 8.

Above that pomt there appear chocolate-coloured shales with beds
of sandstone; and on Little Red Deer River a section (fig. 9) was ob-

4. Sandstones and shales.

d. Septaria-clays.

; height 600 feet.
d. Chocolate-coloured arenaceous shales.

ous shales, with thin seams of coal.

Length 7 miles

the Exterior Range of the Rocky Mountains, on Little Red Deer River.
with coal in thin streaks, and ironstone.

Fig. 10.—Section along Dead-man River, near the Old Bow Fort.
-sandstone.

a. Heavy-bedded clay-sandstones, with streaks of carbon, becoming disturbed and altered.

6. Sharply bedded sandstones and carbonace

Fig. 9.—Section of
c. Septaria-clays.
a
a. Concretionary clay
c. Black carbonaceous shales,

served, in which the sandstone beds become disturbed and harder,
presenting beautiful flexures and exposing at the base the same shales.

428 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

Relations of the Cretaceous Series on the West—On Weepaioos
Creek, a tributary to Deadman’s River, and within fifteen miles
of the Old Bow Fort, thin disturbed beds are very distinctly ex-
posed, as in fig. 10, and must include an enormous thickness of strata.
Although in the absence of fossils I cannot speak positively, yet I
believe that these sections include Carboniferous strata, which are
represented by the lower grits and shales, which contain coal in thin
streaks with plant-impressions. From some of the higher beds at
the Bow Fort, a small Cardiwm was procured. Also on the North
Saskatchewan, over the grits and shales of probably Carboniferous
age, there came beds of pink quartzose grit with dark shales, on
which rested a great thickness of black aluminous shale containing a
small Ostrea in great abundance. Also on the west shore of Lac &
Bruler, where the Athabasca River leaves the mountains, the same
strata were observed resting high up on the flanks of a mountain of
Carboniferous Limestone.

At many other points in the mountains throughout the eastern
ranges, patches of shales occur, highly ferruginous and along with
grits and heavy-bedded sandstones of various tints, and having appa-
rently a superior position to the rocks of Carboniferous age, of which
the greater mass of that portion of the mountains is composed. In
the sections of the various mountain-ranges, the beds which I con-
sider to belong to this group I have lettered a, and, as they are of
great thickness, it is probable that they represent some of the strata
that are found undisturbed in the prairies. In the exterior range
of mountains on the North Saskatchewan, masses of thick-bedded
encrinital limestone rise to the height of 1500 feet with a heavy dip
to the west; while the pink grits and aluminous shales dip away
from them in every direction, just as if they had been masses of
intrusive rock thrust up from below,—thus showing the want of con-
formity between these limestones and the strata that I consider to
intervene between them and the Cretaceous.

Cretaceous Strata of Vancower Island and the Gulf of Georgia.—
The map No. V*. is from the Admiralty-chart of the straits be-
tween the south end of Vancouver Island and the mainland, but
extended northwards so as to include the portion of the coal-mines.
On it I have sketched-in the probable range of the different forma-
tions, but in a very imperfect manner, as my own observations were
only the result of a trip made in a canoe with four Indians for seventy
miles up the coast to Nanaimo. At Nanaimo coal has been worked
by the Hudson Bay Company since 1854, and the total export up to
January 2nd, 1860, has been about 12,000 tons. Through the kind-
ness of Mr. Nichol, the gentleman in charge of the works, and of
Mr. Pearce, of the Land-office, lam able to show a map of the neigh-
bourhood, in which I have inserted my own observations of the
Geology (Plate XIII.). At the time of my visit there were three

* Tt was not thought necessary to publish this map.

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 429

pits in operation, giving employment to thirty miners and a number of
labourers. The former are principally Scotch and Staffordshire men
that have been brought out to the country at the Hudson Bay Com-
pany’s expense, but the greater number of the labourers are Indians,
small tribes of whom come and settle at the mines and work
for a short time until they tire of the uncongenial life, when they
leave to make room for another band. The irregular supply of labour
from this cause adds greatly to the uncertainty and expense of the
workings. When working in the best seams at Nanaimo, a miner
can put out 21 tons per day. The shipment from Nanaimo in the
month of January 1860 was 2000 tons, the trade having at that time
been suddenly extended by the demand consequent upon the esta-
blishment of gas-works at Portland, Oregon, and several other places.
This demand was supplied from a large stock that was lying on hand
at the time, but which, from having been exposed to the action of the
weather for many years, was of very inferior quality. In spite of
this, however, I understand that the market has continued steady
throughout last year, and that the coal has been much used in Cali-
fornia for making gas instead of that brought from the Eastern States
as heretofore. Coal from the same description of strata has been
also worked to some extent on the opposite side of the Gulf of Georgia
at Bellingham Bay, and also at Coose Bay in Washington Territory.
Although it has been found in many other localities along the coast,
as I shall mention after describing the formation, these are the only
places where it has been worked to any extent. The whole forma-
tion associated with the lignite- or coal-beds is very extensively de-
veloped along the Pacific coast, and has generally been considered
to be of Tertiary age, excepting from the first accounts sent home,
which, as there were no fossils, induced geologists to consider them
as Carboniferous. Some fossils transmitted to the Jermyn Street
Museum many years ago were first rightly recognized by the late
Professor E, Forbes as being Cretaceous; but the localities were un-
described, and, in the absence of sections, it was impossible to deduce
anything from them regarding the age of the coal-beds.

The observations which I have now to offer respecting these strata
will, I believe, put their age beyond doubt as Cretaceous; but rightly
to understand the value to be attached to them requires me to give
first a sketch of the physical features of the district.

The southern part of Vancouver Island, where the town of Vic-
toria is built, is composed of metamorphic rocks, with occasional beds
of crystalline limestone. This district and also the central portion
of the island, as may be expected from the formation, is everywhere
hilly and even mountainous, with only limited patches of fertile soil
in the valleys. However, the scanty soil on the rocky hills supports
a fine growth of timber, so that they are almost invariably wooded to
their summits. In the immediate neighbourhood of Victoria there is
nevertheless a good deal of fine open land dotted with small oak-trees.
On passing to the north through the Canal de Haro, the islands of
the archipelago between Vancouver Island and the mainland are seen
to be composed of strata of sandstone and conglomerate, which form

26

430 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

lofty cliffs overhanging intricate but beautiful inlets. The junction
between these two formations was not observed, but I think it is south
of San Juan Island, thence crossing to Vancouver Island by Sannich
Point, and northwards a little way back from the coast, leaving a
narrow strip of fine land*.

These sandstone and conglomerate strata have a uniform strike
from N.N.W. to 8.8.E., and, in passing along the shore of Saturna
Island, they were observed to form several well-marked synclinal
troughs, and on passing through the Plumper Pass to dip gently to the
N.E. under the waters of the Gulf of Georgia. The nature of the
beds was not ascertained beyond the general fact that they are thick-
bedded sandstones and conglomerates, and sometimes strata of clay-
shale. The sandstones are much acted on by the weather, and at
the water-line the sea has generally worn in them caves and hollows.
The conglomerates form the highest beds of the series, and are of
immense thickness.

After passing the Plumper Pass, in proceeding north through Trin-
comalee Channel, Galiano Island to the west presents cliffs, about
800 feet high, of the sandstone and conglomerate, with a gentle dip
to the east ; and sometimes spits or low promontories of the strata
run parallel with the coast, enclosing narrow bays. The west side of
the channel on Salt Spring Island is a low shelving coast heavily tim-
bered to the water’s edge, and exposing outcrops of grey and blue clay-
shales, which dip to the east. The portion of this island which is
occupied by these shales is the finest land for settlement I have seen
on the coast; but the southern part is mountainous, rising to the
height of 2300 feet. It is on the north part of Salt Spring Island
that the saline springs are situated from which it gets its name.
They seem to escape from the shales, and occur in spots clear from
timber and covered with green moist vegetation abounding in sali-
ferous plants. Round the orifices from which the brine escapes, there
have formed conical mounds of granular calcareous sinter stained with

* T am informed by Lieut. Roche, R.N., that, when stationed on that coast, he
discovered a copper-lode, and detected it on Moresby Island and various points
in a line running 8.E. by E., as indicated on the map. I have not myself seen
the samples he brought away, but copper in the metallic state is known to exist
in quantities further north, and I have a specimen of the sulphide of copper
which was said to have been found by the Indians on the mainland. There is no
doubt that a careful examination of Vancouver Island and the adjoining main-
land for metallic veins would yield valuable results. Since my return to England
I have heard that the same silver-ore that is found at Washoe, and that raised such
a furor in San Francisco a year ago, has also been found on the mountains of
Fraser River. The Cascade range of mountains may be looked on as the con-
tinuation of the Sierra Nevada of California, and the marked change in the
nature of the coast-lme north of Wancouver Island shows where the chain
begins to dip down to the sea-level; so that what were formerly mountain-valleys
are converted into inlets and straits. This is a most important physical feature,
and the great facilities for access to the mineral wealth of the country which it
affords will exert a powerful influence on the destinies of British Columbia,
although at present, in the absence of roads, its iron-bound coast and want of
rich flat country are erroneously considered as a bar to its development. Sooner
or later it will be seen how wonderfully this new colony is adapted by nature for
mining, fisheries, and commerce.

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 43

iron; but in summer there is said to be an abundant deposit of pure
white salt.

North of Salt Spring Island the strata preserve the same strike
and general appearance all the way to Nanaimo, the island forming
long spits of sandstone and conglomerate with precipitous shores to
the west. Just below the “rapids” the shales were again noticed,
resting on the sandstone, and both dipping to the west. At very low
tide a thick seam of lignite is exposed at this point and on the island
opposite, and to the east I found a thin seam in the sandstones. At
Nanaimo the sandstone country occupies a broader belt along the
shore of Vancouver Island than further to the south, but immediately
to the north the strike changes to nearly east and west on Newcastle
Island ; and on Fossil Point the lowest beds were seen to rest on igne-
ous rocks, which continued to occupy the coast for the few miles I
went further to the north. At the head of the Gulf of Georgia, the
sandstones again form the islands that crowd the narrow channel
that separates Vancouver Island from the mainland, and also a
ereat extent of both shores. From Comux and Valdez Inlet, which
are situated in this locality, some of the fossils which I have were
procured by Mr. McKay, of the Hudson Bay Company. Also at the
extreme north end of the island, at Fort Rupert, Mr. Lord, of the
Boundary-commission, observed the sandstones and thick beds of
lignite dipping out to sea.

At many points along the eastern shore of the Gulf of Georgia,
these strata have been detected with the associated lignite-beds.
North of Howe’s Sound the mountains closely hug the sea-coast, but
south of that they retire along the north shore of Burrard’s Inlet to
the south-east, so as to be sixty miles inland where the boundary-line
meets them ; thus leaving a very heavily timbered track, which forms
the only level country in British Columbia west of the Cascade Range.
Most of this district is covered by shingle-terraces and other super-
ficial deposits which obscure the underlying strata, but from Burrard’s
Inlet, eight miles north of the entrance to Fraser River, coal and
sandstones containing fossil leaves have been sent home by H. M. S$.
“ Plumper.” Also on Fraser River near Fort Langley, and on its
tributary Pitt River, the coal has been observed, and then again at
Bellingham Bay, south of the boundary-line; so that it is probable
that these strata underlie the greater part of this region.

Details of the Strata at Nanaimo.—In the section, fig. 3,
Plate XIII., I have represented the whole beds observed at
Nanaimo in their probable order, but I did not see any one section
giving the complete sequence expressed in it. Starting from Fossil
Point, north of Departure Bay, we have the high promontory formed
of trap, resting on which are beds of greenstone-conglomerate, con-
sisting of spherical masses of greenstone, cemented by a felspathic
matrix. Over this is a tufaceous bed (with imperfectly formed
erystals), 5 to 6 feet in thickness, partly fused and often pierced by the
trap from below. Then follows a very tough green sandstone quite
filled with shells, for many of the specimens of which I am indebted

to Mr. McKay.
262

432 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

The following is the list as determined by Mr. Etheridge :—
Trigonia Emori.
Trigonia (sp.).
Cytherea Leonensis. (This is the

Exogyra (2 species).
Ostrea (2 species, one of which is
of great size).

most common shell.) Rostellaria.
Arca (3 species). Psammobia (?) sp.
Pecten *.

In speaking of the beds on Red Deer River, I referred to the fossils
found at this place as showing the existence of forms which are in
Mexico associated with those of the Saskatchewan, and in every case
found in the proximity of the lignite-beds. Thus in particular we
have Cytherea Texana, common to the Saskatchewan and Mexico,
and Trigonia Emori, common to Mexico and the Pacific coast. This,
owing tu the very imperfect state of our knowledge and the limited
extent of the collections, is probably to be considered as merely an
indication of the agreement that may yet be established. The green
sandstone beds at the base of the series which contain the lignite
seem to have been deposited originally on the surface of the igneous
rock, which was probably submarine, so that its surface, chilled by
the water, easily broke up into the masses that compose the con-
glomerate-like breccia, the cement of which has been derived from the
tufas that were deposited on its surface. On the shoal thus formed
the greensand beds had been deposited, enclosing the molluscous
remains. The whole has since been repeatedly disturbed, and some
of the lower beds have undergone partial fusion by more recent out-
bursts.

The sandstone is sometimes quite horizontal, but at others quite
vertical for a little way, and is only found as patches all round the
promontory and north side of Departure Bay.

Three hundred yards from the shore in the channel that passes
between Newcastle Island and the Fossil Point, is a row of islands
composed of very fine conglomerate that might be termed “ gravel-
stone,” in beds that dip 8.S.E. at 15°. These beds contain small
fragments of carbonized wood.

A quarter of a mile further on, in the direction of the dip on the
north end of Neweastle Island, there are high cliffs of sandstone,
which preserve the same direction. They seem to be rather more
disturbed than the strata that form the islands in the channel, but
this appearance is exaggerated by the great amount of false bedding.
The strata of sandstone continue to preserve the same direction of dip
all along the coast of Newcastle Island, but gradually becoming
more horizontal towards the southern extremity. On the west side
of the Island at Exit Channel occur the seams of coal, the lowest of
which has been worked to a considerable extent, while the existence
of the other has only been found by boring. The outcrop of these
two seams has been ascertained on the east shore of the island, where

* It is probably from this place that the fossils were procured to which Meek
and Hayden refer in a notice of the coal of the Pacific coast, contained in the
Pacific Rai]. Rep. vo!. vi., where they say that among the fossils from Vancouver

Island a number occur in a green sandstone matrix, which have a strong Jurassic
aspect

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 433

they have the same characters and relative position, thus showing
that they are continuous to that extent. The lowest bed of coal is
called the ‘“‘ Newcastle seam,’’ and is worked by levels driven into
the outcrop as it rises with the high bank from the shore. The
coal or lignite is 6 feet thick, with a floor of sandstone, and a roof
of avery tough conglomerate of very small pebbles. The strata have
a dip of 20°, so that the method employed succeeds well for taking out
small quantities.

This mine was not being worked when I visited it, but there were
large heaps of the coal, waiting for a market, that had been lying
there for some years, so that I could judge the effect of the
weather on it with great facility. The surface was turned to a
rusty brown, and the masses showed a tendency to break up with a
slaty fracture—otherwise the exposure had worked but little change.

Along the shore of the island to the south, the strata of argil-
laceous sandstone are seen to dip steadily in the same direction
with less and less inclination, until at the southern extremity they
are almost horizontal. On Douglas Island there is said to be
another seam of coal, from the shales associated with which the fossil
leaves are generally procured. I had not an opportunity of visit-
ing it, however. On the coast at Nanaimo Harbour the strike of
the strata is quite different, but yet they preserve the same character
and sequence, Exit Channel seeming to mark a great fault. The
little peninsula on which the Hudson Bay Company’s establishment
stands, and where the coal was first discovered, is also another
dislocated portion of the strata, as may be seen by reference to the
map.

At Nanaimo, as on Newcastle Island, there are two seams, the
«« Newcastle ” and the ‘“ Douglas,’—the first of which is everywhere
about 6 feet in thickness, with sometimes a floor of fire-clay, but
more generally of sandstone, and the roof consisting of the fine con-
glomerate bed, about 60 feet thick, on which rests the Douglas
seam with an average thickness of from 34 to 4 feet. The roof of
this seam is sometimes of iron-clay-shale, but more often of the
same tough conglomerate that it rests upon. On Chase River, 14
mile to the south, the outcrop of a seam has been discovered and
worked to a small extent, which they consider to be the “‘ Newcastle
seam ;” and as it occurs right in the line of strike, and as they have
ascertained the outcrop at several points, it is probable that the
beds of coal are continuous.

In the mines they have met several “ stone-faults ” or “swells,”
where the floor rises up and throws the coal-seam out for several
fathoms. It is generally represented, however, by a carbonaceous
parting. These faults are a source of great expense in the working, as
the conglomerate to be pierced is exceedingly tough and compact, so
that the blast only brings it away in small pieces.

In proceeding along the coast towards the mouth of Nanaimo River,
the strata consist of argillaceous sandstones with a similar character
to those of the southern part of Newcastle Island, and preserving a
steady though gentle dip to the K.by $8. A short way above the en-

434 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

trance to the river, in the sandstones, there is a thin seam of coal, the
position of which was pointed out to me by Mr. Nichol, as the river
was too high to allow us to see it. Continuing to ascend the river,
which is of small size, we found low exposures of the sandstone still
with the dip to the E.; and at Fossil Bank, three or four miles from
the mouth, they are overlain conformably by dark-purple clays filled
with septaria, which yield Cretaceous fossils. The dip of the beds
is 10° to the E. by N., and the clay strata were clearly seen to rest
on the hard-bedded sandstones.

I found Imoceramus, Baculites, and some other fossils, of which
other specimens are also among those obtained by Mr. Bauerman
at this place. I was told at Nanaimo that Ammonites have frequently
been found there of large size, and from Mr. McKay I got a
number of fossils, some of which he obtained at this locality; but
others having the same appearance, and also contained in septaria,
he procured from Comux and Valdez Inlet at the head of the Gulf
of Georgia; but these two sets of spedmens had been unfortunately
mixed together. For a couple of miles the Nanaimo River flows
through these clay strata, and then turns again from the S.W., and
in ascending the sandstone strata were again found to recur as in
the lower part of the river, but with a more rapid dip. At the
““Canon’’ these sandstones form precipices about 100 feet in height,
bounding a narrow gorge 600 yards long, through which the river
flows. The beds dip at 15° to the E.N.E., and are very like those
of Newcastle Island.

From under these sandstones, in ascending the river, hard beds
of the gravel-conglomerate cropped out with great regularity, sepa-
rated by soft beds of red and greenish clay. These probably corre-
spond to the group with the coal at Nanaimo, but I failed in finding
any proof of it beyond fragments of carbonized wood. The strata
from Fossil Bank up to the river, as far as I went, are shown in
section No. 3, Pl. XIII.

The total thickness of the beds from the coal to the clays at
Fossil Bank I estimated at 600 to 700 feet, but I had no opportunity
of making any exact measurement. Between Nanaimo River and the
coast, there is a tract of very fine country, and it is probably occu-
pied by the Septaria-clays, which, as I mentioned before, were seen a
little south of the rapid.

The following is the list of fossils from the Septaria-clays, which
includes those specimens obtained by McKay from Valdez Inlet :—
Tnoceramus (?) (thisis the J. Crepsi of Conrad and Roemer), L. Tea-
anus, I. Nebracensis, I. unduloplicatus, I. confertim-annulatus, I.
mytiloides, Baculites compressus and two other species, Ammonites
geniculatus and three other species.

It is thus evident that the group of strata with the lignite-seams
towards their base nust be of Cretaceous age; but as yetit would be
premature to infer the exact position which they hold with reference
to the rest of that system. The great beds of conglomerate which
form the long narrow islands along the west of the Gulf of Georgia
must, I think, overlie all these strata.

1861. } HECTOR—ROCKY MOUNTAINS, ETC. 435

From the sandy shales associated with the lignite, I forward frag-
ments of Yew-like fronds, just the same as those I got in the shales.
At the Rocky Mountain House, and in the collection sent home by
H.M.S. “Plumper,” all the specimens from Nanaimo are of this plant.
Those from Burrard’s Inlet are in a different stone, are reticulate
leaves, and were also found along with beds of coal; but there seem
to be no specimens of the Yew frond from that locality*.

From Nanaimo Mr. Bauerman has also sent home a plant that
looks much like a portion of a monocotyledonous leaf.

At Bellingham Bay, sections taken by Mr. Pemberton show that
the lignite occurs in a large quantity at that place. Lieut. Trow-
bridge in describing the strata there says, they are 2000 feet thick,
and inelude, in all, 110 feet of the lignite-ccal. His sections are pro-
bably, however, all of the same group of strata, taken at different
points in the strike, which gives rise to this apparently enormous
thickness.

The analysis of the coal from Bellingham Bay, which is generally
considered inferior to that of Nanaimo, is given in the Pac. Rail.
Report, vol. vi. p. 65, as follows :—

Carbontee er aa 47°63
BiGUMen Lie ee eee: 50°22
J\ Shabana SCs ah 2:15

100-00

This coal has been sold in San Francisco market at from $18 to
$22 per ton (75s. to 91s. 6d. sterling).

Lignite-coal has also been worked for the same market from Coose
Bay, and has the following composition :—

Carbomtyn 20 eOoran: 46:54
Gaseous matter...... 50:27
AISNE oe cpu event ea ae 3:19

100-00

Conrad states that shells from this locality are of Miocene age.

At Benicia, above San Francisco, coal also occurs, and was
wrought for some time, but the dip was too steep.

In Newbury’s Report on the geology of this part of California, I
have not seen any notice of where this Benicia lignite occurs in his.
sections ; but between Benicia and the sea he describes 3000 feet of
strata, the lowest beds being of sandstone and shales resting on, and
penetrated by, serpentine and trap (the same which are so highly
charged with ores of copper and mercury further to the south).
These are followed by green and brown shales, coarse soft sandstone,
fine sandstone and shales, with Pecten, Natica, Mactra, and Tellina,
and these by conglomerates and tufas, the whole lying at an angle of
30°. Towards Benicia are thin-bedded clays with Sharks’ teeth. Up
Feather River, a tributary of the Sacramento River, at Chico Creek,

* Dr. Hooker has specimens from Disco Island, in the arctic regions, where a
Yew frond and angiospermous leaves are associated in the same hand-specimen.

436 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

a calciferous sandstone is described, containing Nucula, Mactra, and
other Tertiary forms; but from the same place are Baculites, Inoce-
rami, and Ammonites, which Meek considers as proving the existence
of Upper Cretaceous strata at that place. So that it is probable that
there are strata of both ages, but included in the same disturbances ;
and it is not unlikely that the section from Benicia to the sea may
also include Cretaceous strata*.

The existence of coal or lignite on the Pacitie coast, of quality fit
for the purposes of raising steam, is of great commercial importance,
and that obtained from Nanaimo is as yet admitted to be the best
in the market. If these beds are therefore discovered to be per-
sistent, so that they can be worked to advantage on a large scale,
there is little doubt that this coal, even though it be an imperfect
substitute forthe finer coal to which we are accustomed in this country,
will form a valuable source of wealth to the new British colony.
Already it is extensively used by the British navy on that station,
and it was found to require only a slight modification in the method
of feeding the fires to make it highly effective as a steam-generator.

As beds of coal of similar quality exist in the Islands of Japan and
Formosa, we should thus have the supply of fuel at the extremities of
the line of the great sea-voyage, if the route from England by the
Canadas, Saskatchewan, and British Columbia to China and the
East were adopted—a natural fitness not to be overlooked in con-
sidering such a scheme.

PALZOZOIC ROCKS OF THE EASTERN AXIS.

The general structural features of the country travelled over on
the canoe-route, so far as they can be learned from a single line of
traverse, have already been well described by Mr. Keating, Sir John
Richardson, Dr. Bigsby, and others; but, from the complicated rela-
tions of the rocks of which it is composed, no detailed observations can
be of any value until they are extended in every direction by means
of a combined topographical and geological survey.

The whole of this district is occupied by a primitive axis—the
‘intermediate primitive belt’? of Sir J. Richardson—which is com-
posed of gneiss, mica-schist, crystalline limestones, and other meta-
morphic rocks, with intrusions of granite, probably of very different
ages, the whole formation being the Laurentian series of Logan, cor-
responding, it is thought, to the fundamental gneiss recently described
by Sir R. Murchison as underlying the most ancient strata in Scot-
land.

From observations made in the course of our journey, it appears
that there are two distinct directions of strata in the rock which
compose this axis, marking it into two districts, one from Lake Supe-
rior to Rainy Lake, the other from Lake of the Woods to Lake Win-
nipeg. Not only the general strike of the altered and upheaved rocks

* On the Colerado River the Texas lignite or coal, in beds 4 feet thick, has been
observed in strata under those with Eocene fossils, and on a tributary of the Del
Norte, beds, 3 to 4 feet thick, occur of good working quality, in true Cretaceous
strata. (Pac. Rail. Rep. vol. vi.)

ROCKY MOUNTAINS, ETC. 437

1861.] HECTOR

in these two districts, but also the direction in which the water-
courses affect the principal descents, and the manner in which the
lakes in each of them are arranged, all indicate a different direction
of the elevating and disturbing force ; in other words, two different
axes of dislocation.

These seem to converge towards the south, including an angle of
about 25°; the eastern one being directed from the north-east to
south-west, while the western one lies much more nearly north and
south. In each of these there is a great central district where
nothing but rounded bosses of granite are seen occurring as ridges
and islands, which rise little above the level of the flooded country
in which they occur. On either side of these two granitic districts
metamorphic rocks are ranged with great irregularity as regards
their order and dip, but still, on the whole, preserving their direction
very consistently with the bearing of the axes to which they respect-
ively belong. ‘There are besides many minor outbursts of granite
oceurring as dykes and intrusions, but they do not seem to interfere
with the above-mentioned general bearings of the country.

From this cause, in crossing the district between Lake Superior
and Rainy Lake, the summit-level is reached by an abrupt and rapid
ascent in a direction at nearly right angles to the main eastern axis.
Then follows a long traverse, almost along the summit of that axis,
and then an abrupt but comparatively short descent to Rainy Lake,
again at right angles to the axis.

The first great step in the ascent from the east is made at the
Kakabica Falls, where, from a succession of faults which mark the
commencement of the more highly metamorphosed rocks, a sudden
elevation is effected, the summit-level of which is 179 feet above
Lake Superior at Fort William.

About one mile below the fall a fine section is exposed in the
form of a cliff 130 feet high, crossing the country from north-east to
south-west, consisting of a dark argillaceous schist in thin fissile beds,
from 1 to 2 inches in thickness, very much jointed, and having
many small veins of quartz, and sometimes calc-spar, included both
in the lines of bedding and in the joints. These beds are quite
horizontal, and through their whole thickness the river has cut its
way back to the present position of the fall in a manner similar
to that in which the river-bed below the Niagara Falls has been
formed.

They are supposed to belong to the Huronian series, a system which
is largely developed on the shores of Lakes Superior and Huron,
resting unconformably upon the Laurentian series, and having, ac-
cording to Sir W. Logan, a thickness of 12,000 feet. This large
system, that has not as yet yielded any fossils, and always underlies
the Silurian, has been considered to represent the Cambrian.

On the River Kaministoquoiah above the fall at Friar’s Portage
the strata have an almost vertical position; and a little further on, at
Lower Island Portage, are found to be dipping at an angle of 40° to
south-south-east, and to be changed in character, having mica deve-
loped in them, and also a great abundance of quartz-veins. Imme-

433 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

diately afterwards, in the course of the ascent, true granite occurs,
and after several alterations schistose flags reappear at Upper Island
Portage, but now dipping at a high angle to the north-west.

From the falls to the Dog Lake the ascent of the river pursues a
northerly course, crossing the beds obliquely by a succession of
minor falls, giving rise to scenery of unequalled beauty. At the
Dog Portage another sudden rise takes place in the water-level ; for
the rocky high grounds which, for a long way below, have been
skirting the river at some distance, forming, as it were, the limits
of a wide valley, here converge and form a granitic barrier across
the river, the summit of which is about 719 fect above Lake Su-
perior, and 440 feet above the river at the lower end of the portage,
but only 140 feet above the lake-level at the upper end, thus making
a rise in the water-level of 297 feet in the short distance of two and
a half miles. As the portage-road passes right over the top of this
hill and leads to a point in the lake far from the exit of the river,
the nature of the rock at the falls which produce this sudden
change in level could not be examined, but the mass of the hills
seems to be granite. Although this is not the highest point of land
over which we passed during the route, still it is probable that this
hill is as high as any portion of the rocky axis of the country; as
those along the lake are inferior to it in elevation, while the
ascent which is made after leaving the upper end of Dog Lake is
through a swampy country covered with drift. In fact, after leaving
Dog Lake, until a considerable descent has been made to the west, no
rock is exposed, the whole summit-level being covered with a thick
deposit of drift.

From the Lake of the Thousand Isles, where the rocky flooring of
the country is again uncovered, until Sturgeon Lake is reached, the
descent is very slight, and the route follows a chain of small lakes,
which are in most cases detached from one another, being sepa-
rated by rocky barriers over which the canoes and cargoes are
carried,

In many cases the lakes are at exactly the same level at each end
of the portage, and the greatest difference between the two ends
of any of these portages is only about 35 feet, so that the total
descent in this part of the route cannot amount to very much. This
chain of lakes may, in fact, be considered as occupying a line parallel
with the summit of the watershed, and the country in which they
lie is almost wholly composed of granite, occurring in broad round
eminences, nowhere rising to 100 feet above the level of this half-
drowned country. It is probable that this granitic belt is expanded
considerably where the old portage-route crosses it, and that the
whole chain of lakes between Lake Rasiganagah and Sturgeon Lake
lies within it. It is this belt which will form the great obstacle to
the formation of any kind of road across this watershed.

From Sturgeon Lake to Bad River there is a considerable descent
to the south, which forms the only exception to the general north-
westerly descent of the waters to Rainy Lake.

From the Lake of the Cross to Lake Namucan the descent is rapid,

1861. | HECTOR——ROCKY MOUNTAINS, ETC. 439

and the river-channel crosses the strata of gneiss and bedded green-
stones at right angles, following the direction of the dip.

Rainy Lake has its length agreeing with the strike of the strata,
which is here more nearly east and west than before.

Between Rainy Lake and the Lake of the Woods the superficial
deposits again cover all rocks from view, and when the north end of
the latter lake is reached and they are again exposed, their general
strike is now changed to almost north and south, agreeing with the
greater axis of the lake, just as Rainy Lake agrees with the strike
of the eastern district. The descent from the Lake of the Woods to
Lake Winnipeg is by successive groups of falls, between which the
river forms lake-like expansions, which he generally at right angles
to its main course.

The first part of the River Winnipeg fiows across vertical strata,
and then enters a granitic district very similar to that passed through
between the Lake of the Thousand Isles and Sturgeon Lake.

The strike of the rocks in this region is generally a little to the
east of north, and the nature of the strata is very similar to that of
the country east of Rainy Lake, but less disturbed by dykes.

No trace was observed of the existence of the schistose rocks on
the west flank of the axis, the gneissose rocks continuing for the
whole way to Lake Winnipeg.

Silurian Rocks.—Myr. Hind, who had favourable opportunities,
from having coasted along Lake Winnipeg and the other lakes that
lie in this formation, gives an interesting account of its development
in his recent work (‘Canadian, Assineboine, and Saskatchewan
Expl. Exped.’ ch. xxxvii.): his fossils having been submitted to
Mr. Billings of the Canadian Geological Survey, the following groups
were identified as occurring in the Winnipeg basin ; all of them are
Lower Silurian:—

1. Chazy Formation. 3. Trenton Limestone.
2. Bird’s-eye Limestone. 4, Hudson River Group.

Of these I only saw the last at the same place that Dr. Owen
examined and recognized the proper age of the bedsin 1848-—namely,
at the Lower Fort Garry on Red River. Here there is a bench of
magnesian limestone exposed in the bed of the river when the
water is low, and which is then quarried for building-purposes. As
the river was high when I was there, this section was not visible,
but from fragments lying on the bank the following fossils were
obtained :—

Cyathophyllum. Ormoceras Lyonii (Séokes).
Columnaria alveolata (Hall), Strophomena plano-convexa.
Favestella (Favosites basaltica of D. Orthis ; var. of O. Lynx.

Owen). Spirifera elegantula.
Receptaculites occidentalis (Sal¢er). Maclurea.

Rbynchonella incubescens (Had/).
These fossils have been named for me by Mr. Salter, who has
kindly examined the few paleecozoic fossils that were procured. 'The
limestone is suberystalline, of a light-buff colour with purple blotches,

440 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 10,

very hard, and having an angular fracture. At Stony Hill, about fif-
teen miles north-west from the upper fort, there is an isolated bluff
of limestone rising from the plain-level to the height of 80 feet.
The south and western exposures are abrupt and waterworn, it
having evidently been at one time an island; and indeed during the
great floods which have several times inundated the settlement it
has been one of the few spots upon which the inhabitants can take
refuge, reaching it by means of boats. The beds of limestone are
horizontal or nearly so, and are slightly different from those at Fort
Garry in their mineral aspect, having a more crystalline structure
and the colour being of a reddish hue. No fossils can be discovered
in newly fractured portions, but on the weathered surfaces a few
obscure remains of fossils are to be seen projecting, together with
siliceous and gritty particles, from a dull floury surface.

The Silurian rocks have now been traced continuously from Lake
Superior west of the sources of the Mississippi, and thence into the
valley of Lake Winnipeg and on to the Arctic Ocean, skirting the
more ancient axis. On the shore of Lake Winnipeg they have been
observed much disturbed and even vertical by Dr. Owen (‘ Report on
Geol. of Minesota,’ &c.), but in general they rest nearly horizontally,
or with only a very slight dip.

Resting on the Silurian strata, Mr. Hind has detected limestone
with Devonian fossils in a tract to the west of Lake Winnipeg, where
there are copious salt-springs, the brine from which is used for the
manufacture of salt. He considers the line marked by the occur-
rence of these salt-springs to indicate the outcrop of the Devonian
strata.

The route of the Expedition at once passed from Silurian to Cre-
taceous rocks without any indications of the intervening formations
until reaching the Rocky Mountains.

STRUCTURE OF THE ROCKY MOUNTAINS.

Physical Character—The plains at the eastern base of the Rocky
Mountains are, as I have before stated, elevated above the sea 4000
feet; and, as the average limit of vigorous vegetation in that latitude
is attained at 5000 to 6000 feet, the greater mass of the mountains
displays in consequence naked and bald surfaces, which are generally
very precipitous. Their structure is thus easily discerned to be of
strata the real thickness of which, originally very great. has been
much exaggerated by the complex flexures which cause the beds to
recur again and again, sometimes even in the same mountain. The
apparent confusion is so great from this cause as to strike the eye
at once, and it is not until observations have been made over a con-
siderable extent of the range that the extreme regularity with which
the disturbing agencies have been exercised becomes evident. The
flexures of the strata on the eastern part of the mountains have
been so completely inverted that the prevailing dip is towards the
centre of the mountains—that is, to the W. and S. The strike of the
plications varies, but in a regular manner. From Bow Fort, south-
wards, it is only a few degrees east of south ; but north of that river

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 441

to the valley of the North Saskatchewan its average direction is
8.S.E., and between that valley and the Athabasca it is 8.E. nearly,
while to the north of that it is changed to within two points of east
and west. These changes in the direction of the strata take place at
the different great valleys by which these rivers leave the mountains,
and which probably mark the lines of transverse fracture. The
mountains are divided into groups by great longitudinal valleys,
which are met with in every part of the chain that I examined,
running in the length of the range and forming a part of each of
the river-systems. The course of these rivers is, therefore, in every
case zigzag, alternately flowing through wide valleys either to the
north or south, and then making short breaks to the east or west
through narrow and rugged defiles.

Throughout these great valleys it seems to be the arrangement of
the detrital deposits that has in many cases determined the direc-
tion in which the rivers flow.

A curious feature is to be remarked in tke position of the water-
shed between the waters of the Pacific and those of the Atlantic,
arising, no doubt, from this cause. It is found gradually to occupy a
position further to the west, and through the chain, so to speak, as
the rivers rise more to the north.

Thus the Missouri can hardly be said to rise within the Rocky
Mountains atall. Belly River, on the boundary-line, rises from the
first ridge before reaching the first longitudinal valley. Kana-
niskis River rises in that valley, or from the second range; Bow
River from the third range; the North Saskatchewan from the
fourth range; the Athabasca from the fifth; and, although I have
not seen Peace River, the one further to the north, still this feature
is so well marked that it has been spoken of as rising on the west
side of the Rocky Mountains and then cutting through that range
to the east. This all tends to show that we must not look on the
Rocky Mountains as a continuous range, stretching as a line of frac-
ture through the length of the continent, but rather as a succession
of centres of disturbance, a fact which has been amply proved within
the American territory.

Thus what are known as the Rocky Mountains at the head of the
Missouri are rounded off to the north and south, losing their charac-
ter of a lengthened range in that of a mass of mountain-country.

In like manner the Rocky Mountains within the British territory
must be looked upon as a mass with its longer axis lying N.N.W.
and 8.8.E., with which the main strike of the strata conforms.

Geological Structure.—There are three of these great longitudinal
valleys that are more persistent than the others, each of which marks
a change in the formations which compose the mountains. As far
west as the first of these, the structure of the mountains may be
understood from the sections*, figs. 11 G12. The strata are of thick-
bedded limestones, These limestones are of dark and lght-blue

* All these sections are merely diagrams combining the results of detached
observations.

[Apr. 10,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

442

ine, compact, or cherty, with fossils that are of Car-

colour, crystall
boniferous age.

In the sections these limestones are lettered bd.

oplueig ff ‘S}STIOR *a ‘a
if a

ws =, eau ee
er eS =~
a oS,

H
1
t
care rs 1
1
4

“"soye] Jo[pprg *suIeyUNo], a1uej00¥f H

*AaTTBA BIQuIN[OD *ssvq Ausaqovlg “purl Jo yy S10 fF]

‘sumpunozy hysogy ayy fo adojy ysaq4 ay fo woyng—FT Biz

“eyeays (4) UeLINTIG “p “ByBYS UBIUOAA(T “9 9 "BYBAJS SHOLOFTUOGARD *¢ Q "SO[BYS-BA.8Q PUB L{V.YS OLOZOSOT, “YD
7) D D

2 Pp Ba q D

‘aSuey puossg ‘aBunyy sry “aA daays ‘adury s
‘sumpunozy hyooy oy myn ‘wamay Unmayonysny Yon 2y7 Huopy woyng—zy *Stiq

nvazvig

‘SUTIOA-Z].1ENb TIM SoqvIS BsooTVy, *a

(4 UBLINTIg) soyeroUMO[Fu0d pure sozIZjAeN’y “p
"BIVAYS UBIUOAD(T °9

_ “ByBAYS SNOLOFTUOGARD “9 “BYBIGS OLOZOSOW, "VD

DM

‘odury pequeg ‘aZuey puovas ‘aduvy 4811 W104 Mog

‘seappunozy hysoyy ayn mynm wang mog buojn wonvgy— Ty “Buy

‘syood (¢) URLINTIg “p "BIAS WRINOADET *0 “BYBAYS SNOLOJIMOGILD “Q
cc) a i a

Along with them are softer beds of gritty sandy shale, generally of
a dull-red or purple colour; and the irregular disintegration of these

1861. ] HECTOR—ROCKY MOUNTAINS, ETC. 443

two groups of strata produces the rugged appearance of this range,
the mountains being in general formed by masses of synclinal folds,
while the valleys mark anticlinal fractures. The valley between the
first and second range marks a great trough in the strata in which
patches are preserved of chocolate-coloured ferruginous shales with
beds of grit and layers of ironstone, and which are the same seen in
the above sections resting on the flanks of the limestone mountains,
belonging to a more recent formation, and to which I have previously
alluded (p. 427). In the second range we have the same limestones
and shales repeated as in the first; but at the base I observed traces
of a magnesian limestone of a buff colour, containing Atrypa reticu-
laris, a true Devonian fossil (¢, fig. 11). Towards the west this range
everywhere in the mountains presents a sheer wall of vertical lime-
stone, the ragged edge of the beds forming the Saw-back Range.
The change in the look of the mountains that now takes place may
be well seen, as on Bow River in fig. 13, where the east side of this

Fig. 13.—Sketch of the Second Great Valley, on Bow Rver,
im the Rocky Mountains.

valley consists of vertical strata, while on the west side the moun-
tains are formed of cubical masses of strata that are almost horizontal.
These are of hard quartzite-sandstone, passing into conglomerate,
and capped by hard limestone, with the ferruginous shales resting
obliquely on their sides at the line of fracture. At the source of the
Pipe-stone Creek the mountains form part of the second range,
and there I procured some fossils that have been distinguished by
Mr. Salter as Orthis, Lingula, Euomphalus, and from the limestone
Lithostrotion, which are either Carboniferous or Devonian. On
the Athabasca River gneissoid rocks, traversed with quartz-veins,
were observed to form the floor of the second longitudinal valley, and
in descending the valley of Vermilion River, and also that of Blae-
berry River, talcose shales were met with also, forming the floor of
the valley (e, figs. 11 & 14). On Kicking-horse River in the third
range, we have the mountains again formed of blue limestone, to-
gether with a compact blue schist with red bands, giving a curious
striped aspect to the rock. ‘This schist or slate-rock forms the
highest points of the mountains in the above district (d, fig. 14).
The third longitudinal valley is that in which the Columbia
and Kootanie Rivers flow in opposite directions parallel with the
range. Along the eastern shore of the Columbia Lakes we find the
mountains again composed of the Carboniferous ihmestones which form
the eastern ranges, but resting unconformably on slates (e, fig. 14).

444 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (Apr. 10,

At the source of the North Saskatchewan the mountains are very
massive, and are principally composed of a deep-blue compact lime-
stone, that often contains nodules of iron-pyrites (c, fig. 14). A few
specimens of Atrypa (reticularis?) and Athyris lead Mr. Salter to
regard these limestones as Devonian. To the west of the great
Columbian valley the strata were only seen in descending the Koo-
tanie River, as shown in the section, fig. 14. That river breaks through
a succession of well-defined ranges that never rise to any great
altitude, and are composed of dark schists (e’), traversed by quartz-
veins, the whole forming beautifully developed flexures. Some
miles east of Padler Lake the slates (e) were again seen underlying
these schists, and at that place commences a district of granitic
country (f), where mountain-ridges rise as rounded masses to the
height of 800 to 1000 feet above the general level.

Towards Fort Colvile the Kullespellem Mountains bound the
Columbia to the east, and are formed of quartzose slates in thin
beds, limestone partly altered, and serpentine. At the south end of
the Kulespellem Mountains the great trap-floes of the Columbian
Plains commence, and are there seen to overlie the granite and other
strata, filling up the hollows in their surface.

The horizontal extent of these lava-floes is truly wonderful, as
they occupy nearly the whole surface of the great Columbian Desert
without any chain of mountains or peaks existing to which their
origin can be referred.

This great plain is frequently cut by chasms 500 to 600 feet deep,
the sides of which expose stratum after stratum of thin lavas inter-
calated with softer tufaceous beds, the whole being quite horizontal.
The lava-floes have often a columnar structure, especially in the
neighbourhood of depressions in the plain, such as Sil-kat-liva Lake,
which probably mark the position of ancient craters. At some points
up Snake River, American parties have procured Tertiary fossils from
the tufaceous limestone that underlies these basalts.

The whole way to the Dalles the Columbia flows through an
enormous chasm in these stratified lavas and tufas, giving rise to
most wonderful scenery. Often the whole of this mighty river is
compressed between perpendicular walls of basalt, but with a
channel of such depth that its treacherously swift current preserves a
glassy surface.

CASCADE RANGE.

Where the Columbia breaks through the Cascade Range there
is a great rapid rather than a fall, from which the moun-
tains have derived their name, and connected with the formation
of which there is an old Indian legend. The river from the
Dalles to this point, a distance of forty miles, is almost without
current, and bounded by a perpendicular wall of mountains on either
hand, and the story is, that at one time the river had a uniformly swift
current the whole way, and that where the Cascades now are, it
then passed under a gigantic natural arch that crossed from side toside
ofthe chasm. During a great earthquake this arch fell down, and
now remains as the chain of islands across the head of the Cascades,

1861.] HECTOR—ROCKY MOUNTAINS, ETc. 445

while the river has gradually carried down the fragments so as to
form the long rapid. The river was thus dammed back all the way
to the Dalles, and submerged the forests along its banks, the stumps
of which are still to be seen sticking out of the water at a distance of
several hundred yards from the shore. The stumps of the submerged
trees are of a species that never grows near water; and as the other
conditions of the story agree remarkably well, I am inclined to think
there may be some truth in it. It was told me, as we were passing
the spot, by a fellow-passenger who had been a long time among
the natives as an American Indian agent; and I have since heard
it from gentlemen who have been twenty-five years in that country
in the Hudson Bay service.

In descending from the Cascades to Vancouver, stratified rocks
are seen perched on the flanks of the mountains, among which
is a group of strata of a bright vermilion colour. Along the valley
of the river there are also strata of tufaceous sandstone and clay
which are only slightly disturbed. At the Cascades the beds attain
a considerable thickness and contain large fragments of silicified
wood. The scenery of the Lower Columbia before reaching the flat
district around Fort Vancouver is exceedingly fine, the river pass-
ing, successively, bold promontories more than 1000 feet in height,
and sometimes under lines of cliff over which rivulets pour as cas-
cades from a height of 600 feet. Between the Olympic or Coast
Range, which stretches to Cape Flattery, and the Cascade Range, the
great valley of Puget Sound is continued south as far as latitude 44°,
first as far as the Columbia River by the Cowlitz Valley, and then by
the valley of the Willamette, and presents a long strip of valuable
country, which forms the only good part of Oregon and Washington
territories. The River Columbia crosses this strip of country, only
Genie to its direction for a short way from Vancouver to the

Jowlitz.

Of the Olympic Range I believe nothing is known; but, as viewed
from Puget Sound, the outline of these mountains reminded me in a
striking manner of that of the exterior ranges of the Rocky Moun-
tains, where they are composed of plications of stratified rocks.

I have previously mentioned the metamorphic rocks, with beds of
crystalline limestone, that form the mass of Vancouver Island ; and
for further interesting details respecting the south end of the island,
reference may be made to Mr. Bauerman’s paper, published in the
Society’s Journal, Noy. 1859.

Apri 24, 1861.

Daniel Mackintosh, Esq., Chichester, and Richard Payne Cotton,
M.D., F.R.C.P. Lond., 46 Clarges Street, Piccadilly, were elected
Fellows.

The following communications were read :—
VOL, XVII,—PART I, 2

446 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,

1. On the Occurrence of the CYRENA FLUMINALIS, together with MaRInE
Suetis of Recent Spxctzs, in Buns of Sanp and Graven over beds
of BoutpEr-ciay near Hui; with an Account of some Bornes and
WELL-sEctTIONS in the same District. By JosepH Prestwicg,
Esq., F.R.S., Treas.G.S., &c.

Few fossils of its class can lay claim to the interest that has at-
tached to the Cyrena fluminalis. This small bivalve shell, described
in 1834 by Mr. Searles Wood as the Cyrena trigonula of the
Norwich Crag, and afterwards identified with the C. consobrina of
Caillaud, now living in the Nile and parts of Asia*, has, from the cir-
cumstance of its occurrence in beds of well-defined position beneath
the Boulder-clay of Norfolk, been ranked as pre-eminently a pre-
glacial shell, and as the associate of the Hippopotamus major and
Elephas antiquus.

On the strength of the paleontological argument, certain isolated
beds containing the same Cyrena, including more especially the well-
known deposits of the Thames Valley, the immediate relation of
which to the Boulder-clay is not apparent, were referred to the same
preglacial period. The late Mr. Trimmer, Mr. Morris, and myself
have, however, always held a different opinion, inclining to the belief
that these latter deposits were of later date than the Boulder-clay.
Our reasons being mainly based upon the general physical phenomena,
and wanting the more positive proof of superposition, the age of these
deposits remained a point at issue between geologists and paleeonto-
logists. But if the determination of age were already desirable on
the abstract geological question, it is now of much more importance
in consequence of the circumstance of the same Cyrena having lately
been found in the neighbourhood of Abbeville in the beds of sand
and gravel containing Flint Implements?.

So much of the paleontological argument as hinges on the occur-
rence of the Elephas antiquus in these beds has lost its weight, inas-
much as this species, instead of occurring invariably in beds beneath
those containing the Elephas primigenius and always apart from it,
has now been found associated with it in positions which leave little
doubt of their original contemporaneity. The Z. antiquus may have
lived before the Z. primigenius ; but it certainly appears to have lived
on to the period of the latter species, which, the evidence I have
collected goes to show, was probably not introduced into this country
until after the Boulder-clay period.

The Cyrena, although found in various beds supposed to be newer
than the Boulder-clay, could not be proved in any of these cases to
be newer by direct superposition. In the course of last summer,
however, I obtained proof of its presence in beds considerably higher,
at all events, than the Mammaliferous or Norwich Crag. I had visited

* See the account given of the range of the living shell, by Mr. Woodward,
in the Zool. Proc. 1856, p. 187.

t The first Cyrena found there I took out of a bed of sand overlying a bed of
subangular flints, in which I at the same time found three flint flakes or knives:
larger lance-head-shaped flint implements have been found in a still lower bed

of gravel adjoining the town-walls. Four more specimens of the Cyrena have
since been found in some sands. (See section in the Phil. Trans. for 1860, p. 284.)

1861.] PRESTWICH—BOULDER-CLAY. 447

Hull and examined the Boulder-clay of the Yorkshire Cliffs, when
my attention was drawn to the single valve of a Cyrena fluminalis,
identical with the Grays species, in the fine collection of organic re-
mains of Mr. Leckenby, of Scarborough, and long known to Mr Morris.
Mr. Leckenby informed me that it came from the shelly gravels
described by Professor Phillips near Hull, where it was not rare.

Returning to Hull and following the instructions given in Prof.
Phillips’s ‘Geology of Yorkshire’ (vol. i. p. 23), I found my way
readily to the gravel-pit, one mile south of Ridgemont near Hedon,
therein described. Professor Phillips gives a list of eight shells
from this locality, and also notices the common occurrence of another
shell which he could not refer to any then described species, and
which proves to be this Cyrena. The sectionis small; and although
the superposition of the beds is not shown, they are justly inferred
by Prof. Phillips to be closely connected with the Boulder-clay.
To the 8.W. of this pit are several old pits, now nearly obscured, to
which I shall revert presently. My attention was then directed to a
large ballast-pit on the Hull and Holderness Railway, one mile 8.8. W.
from the above-mentioned pit, and 81 miles eastward of Hull. There
is no name given to the spot on the Ordnance Map, but locally it is
known as “ Kelsey Hill.” The section at this spot is extremely in-
teresting. It exhibits great beds of coarse gravel and fine shingle
interstratified roughly and irregularly with beds of sand—the whole
of a light colour, and with much oblique bedding. In places there are
no shells ; in other places they are most abundant The following
sections give the general characters of the deposit.

The gravel in the upper Section at the Hast End of the
beds consists of subangular Ballast-pit, Kelsey Hill.
flts with pebbles of the
older rocks, but the latter
are in far larger proportion in
the lower part of the section,
some beds consisting almost
entirely of small boulders of
granite, greenstone, quartz,
porphyry, mica-slate, lime-
stones, sandstones, lias, and
hard chalk, together with
very large flints*. They are
almost all worn and sub-
angular, and many are per-

fectly rounded. Some spe- a. Gravelly soil.

cimens are above a foot in b. pees ce Bai

ee the lime- A Gravel Bee of small rounded
stone blocks retain faint boulders mixed with shells, 5-6 feet.
traces of glacial scratching. e. Light-coloured sands, with shells,
Many of the blocks of chalk chiefly in fragments.

are drilled with Annelid borings and perforated with the holes of the
Pholas crispata. Some few of the rock-blocks and many of the large

* See ‘Geology of Yorkshire,’ 2nd edit. p. 20-23, for fuller details of the
lithological character of the strata. ates
Haz

448 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,

flints, however, are angular. The large gravel, d, contains with the
sand in the interstices between the boulders a certain number of the
shells hereafter named*.

Towards the central part of the pit, now in course of being
worked, the gravel is finer and the shells more numerous and per-
fect. So abundant are the shells and so regular the bedding, that in
the following section the deposit has quite a Crag-like appearance.

Some 3 or 4 feet of a larger and coarser gravel has been removed
from the top of this section.
The shells in 6 are extreme-
ly numerous,—the Yellina,
Cardium, Mactra, Bucconum,
‘a Littorina, Nassa, Natica,
and Purpura preponderating,
with the Cyrena, whichhard-
ly yields in abundance to any
2h of the others. The Anoma,
== Corbula, Nucula, Venus,
Murex, and Fusus are rare.
Almost all the shells are
worn, and have the ap-
Ge = pearance of having been
a. Gravel and sand. dead shells cast up on a
6, Fine gravel and sand, with veins of beach or a bank. ‘The bi-

Gosia stelle valves are more perfect than
ce. Sand and gravel, in oblique layers ; :
andsawith foros chal, ‘ the univalyes, which are for

the most part more or less

broken, especially the large Buccinum. Generally the shells are but
little decomposed, many of them retaining even some of their colour.

Section close-adjoining the Railway at
the Ballast-pit, Kelsey Hill.
S.w. S.E.

Ft. in

I am indebted for the following reyised list and remarks to Mr. J.
Gwyn Jeffreys, F.R.S., F.G.S., &e.
MOLLUSCA.
[These are alphabetically arranged, but according to the nomenclature of Forbes
and Hanley. The species marked with an asterisk are not in their list.]

No. Species. Remarks on the comparative
frequency, &e.

Bivalves.

1. Anomia ephippium ........ Asingle valye,noticed by Mr. Leckenby.
2. Astarte compressa ........ A fragment.
3. Cardiumiedule :). cna. ce Common: the ordinary form,

* Another locality mentioned by Professor Phillips is Brandesburton, 15 miles
northward from Kelsey. J had not time to visit this place, but my friend Mr.
Smith, of Hull, has recently been there, and he reports to me that the gravel
forms a ridge of low hills which have been worked for centuries. At the pits now
open, shells are very scarce. The specimens he has sent me are only worn frag-
ments of Cardium edule, Tellina solidula, and Pholas crispata(?). The locality,
however, is important as showing more distinctly than at Kelsey Hill the super-
position of the gravels in the Boulder-clay ; for at the village a deep well has been
sunk, which, after passing through the lower 10 or 12 feet of gravel, traversed 60
feet of clay with stones (Boulder-clay); below this was a bed of flinty gravel, and
then the Chalk at a depth of about 80 feet.

+ This list is more copious than the one I first gave, and is the result of an ex-

1861. ] PRESTWICH—BOULDER-CLAY. 449

No. Species. Remarks on the comparative
frequency, &c.
Bivalves,
Cardium edule, var......... An estuarine or brackish-water form ;
more produced at the anterior side
and thinner: less frequent than the

last *.

4. Corbula nucleus .......... Rare.

5. Cyprina Islandicat ........ A fragment.

*6, Cyrena fluminalis, Miller .. Abundant. Corbicula fluminalis of
conchologists. Some specimens are
larger than recent ones of the same
form.

dmeactrarsOlidajc tia. sje + 8 Not common: a small variety, inter-
mediate between this species and JZ.
elliptica of Brown, which I consider
a variety of it.

8. subtruncata........ Not common. The lateral teeth in this
and the last species are perpendicu-
larly striated, as in Cyrena.

— FEN obi Rare. The Irish deeply striated form.

Oe Maya strumeatal |). s|icseie ois Two fragments.

HOF eMevitlusiedulige. po .ccc. we i: A few fragments.

ibs IN ienieya elena aa codon 4 A fragment.

We Osirea edulis: 2s... os es « Rather common: not of any size. Ap-
parently an estuarine form.

See Holas/crispata.s.cio2 5... A few fragments.

Awe tellinasolidula, ..004500.2. Very abundant, but not of any size.

ionaVienusistriatula. : <2. .0y sie A single valve.

Umwalves.

16. Buccinum undatum........ Very abundant: a northern form, hav-
ing the ribs more obliquely carved.

17. Dentalium entale.......... Not common.

18. Fusus gracilis, Da Costa.... A fragment. This is the F. Islandicus
of Forbes and Hanley, who appear
to have mistaken Da Costa’s species
for the F. Islandicus of Chemnitz.
These species are very distinct.

antiquus, var. despectus . An immature specimen and a fragment
of another. In this country it occurs
only in the south of Ireland and in
Zetland.

19.

amination just made by Mr. Jeffreys of my original collection, as well as of a fur-
ther series collected by Mr. Smith, and sent me only a few days since. It will be
seen by my observations which follow those of Mr. Jeffreys, and which remain
as they before stood, that our conclusions, which are based upon independent
grounds, are in very close agreement.—2Ist Oct. 1861.

* In Mr. M°Andrew’s Report to the British Association, in 1856, on certain
dredging operations, he says (p. 134), “‘ Near Tunis a narrow neck of land divides
the bay from a shallow salt-water lake, at the head of which the city of Tunis is
situated ; on the one side of this neck of land (that facing the bay) all the speci-
mens of Cardium edule were strong, triangular, and with few ribs, while on the
other side, towards the lake, they were thinner, wider, and much more numerously
ribbed. The northern varieties attain the largest size.’—J. G. J.

+ This may have been washed out of some of the lower beds of the Boulder-
clay, where such fragments are often common. So also the fragment of Astarie
compressa.—). P.

450 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,
No. Species. Remarks on the comparative
frequency, &e.
Univalves.
Fusus antiquus,var.sinistrorsus One specimen, exactly resembling the
common Crag shells. It is very rare
as recent or living in these seas.

20. Lacuna crassior ......:... Very rare.

21. VANCE pete ec os eas onsets Several specimens. One of them is of
unusually large size.

22. Littorina littorea.......... There is only one specimen which I can
refer to this species, and that is not
perfect.

23. ———rudis............6. Only one small specimen.

#24, squalida, Brod. § Sow. Rather common. An Arctic form. It
is the same species as occurs in the
newer Crag strata. Intermediate be-
tween L. littorea and L. rudis. Pro-
bably the Z. limata of Lovén.

25. Mangelia nebula ......... . Three imperfect specimens.

*26. --— pyramidalis, Strém. Two young specimens. A Norwegian
species.

27. — turricula ........ Several specimens.

28. Murex erinaceus .......... A fragment. Neither this, nor Man-
gelia nebula, is known to me as an
arctic species.

29. Nassa reticulata .......... Frequent.

- ————__,, var. scala- .
a ee peta One specimen.

*30. Natica clausa, Brod. § Sow... A few specimens; one is very large.
A northern species.

31 Groenlandica, Beck .. Three specimens—one large—and a

(pusilla, F. 8 ZH.) fragment of another still larger. It
survives on the Doggerbank.

32 helicoidesine os sepa: Rare. Found living with the last on
the Doggerbank.

33 ALL HCG ES Lh apa Ee Seana Not common.

34. Purpura lapillus .......... Very abundant.

30. Rissoa labiosa ............ A fragment.

*36 -— subumbilicata, Mont. Two imperfect specimens. An estua-
rine species, allied to R. ulve, of
which it may be only a variety.

37. Trophon clathratum ...... A few specimens, of large size.

*38. Gunneri, Lovén .... Two specimens; Norwegian.

*39. ———— scalariforme, Gould Two specimens; northern.

40. Turritella communis ...... Two fragments.

Cirrhiped.

Balanus crenatus, Bruguiére. Detached valves are rather common.

Although nearly all of the species comprised in the foregoing list
still exist in the German Ocean, there are some which are only known
as living in more northern seas.

Mr. Jeffreys further observes, “The conditions of coast and sea-
bottom which produced these animals appear to have been as follows.

ee

ist. A muddy estuary, like the Solent, into and out of which

a large river flowed, and in which grew the Zostera marina: this

1861.] PRESTWICH—-BOULDER-CLAY. 451

estuary and river were inhabited by the Rissow, Lacuna vincta, the
variety of Cardium, Tellina solidula, the Oyrena (or Corbicula),
and probably the Ostrea; the shells being carried down into the sea
by the river.

“2nd. Below the beach, referred to underneath, a belt of loose
stones of different sizes, with patches of mud; and here lived the
Purpura, Mytilus, Nassa, Littorine, and Balanus.

«3rd. An exposed patch of chalk, which produced the Pholas.

‘4th, A wide and deep patch of sand with gravelly mud, inha-
bited by the typical Cardiwm, the Mactre, and the Mya. Only un-
covered at low spring-tides.

“Sth. Seaward, at a depth of from 20 to 30 fathoms, and at a
distance of not more than two or three miles from the shore, where
the ground was sandy, we might expect to find the Buccinwm, Fusz,
Natice, Corbula, Nucula, Astarte, Venus, Dentalium, Lacuna ecrassior,
variety of Mactra subtruncata, the Tropha, and Mangelie. All
these were within the range of the tidal current, and may have
been thrown up on a pebbly beach, which would account for their
generally broken and rolled condition.”

In addition to the above I may notice the occurrence of a few
small fish vertebree and of annelid borings in the pieces of chalk. I
was informed that some large bones* had been found two or three
years since; but the only trace of bone I found was an undetermi-
nable fragment reduced to a pebble-form.

As it would appear that none of the shells are in their original habitat,
it becomes a question whether they are all contemporaneous, and of the
same date as the gravel in which they are imbedded. With one or
two exceptions I am inclined to answer in the affirmative. The shells
are alike in mineral condition, and they show the same amount of
wear. ‘They do not seem to have been transported far, or subjected
to very much rolling about. If any had been washed out of an older
cliff, then we should look for more or less difference of wear and of
mineral condition between such introduced specimens and the more
recent specimens ; but no such distinctions are apparent. All the
species, with the exception of the Cyrena, are such as might live in
the same sea, and have the ordinary appearance of dead shells cast
up on a gravelly bank or ona beach. The Cyrena, however, being a
freshwater shell, must either have been washed out of an older deposit
or else carried out to sea from the rivers which it inhabited. With
this fossil also there is nothing on the score of wear and mineral con-
dition to distinguish it from its present marine associates. As these
latter indicate a certain amount of transport and intermingling by
marine currents, the same cause has in all probability operated along
the whole littoral area and caused the intermingling, not only of the
shells of different zones of depth, but also of those brought down by
streams. That there were such freshwater streams in the vicinity

* Professor Phillips mentions the occurrence of the tusk of an Elephant in simi-
lar beds at Brandesburton (Geology of Yorkshire, 2nd edit. vol. i. p. 22).

452 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [Apr. 24,

of this area, is indicated by some of the above-mentioned marine
shells exhibiting varieties peculiar to brackish waters*. It is to be
observed, nevertheless, that no other freshwater shells nor any land-
shells are found in the Kelsey Hill beds; but this may arise from the
strength and solidity of the Cyrena being superior to that of the
ordinary freshwater and land-shells. Its numbers are also remark-
able. It occurs literally in thousands. For these reasons I am
inclined to believe it to have been contemporaneous with the marine
shells with which it is found associated.

With regard to the position of the Kelsey Hill gravels, the coast-
section from the Humber to Bridlington shows cliffs of Boulder-clay
capped here and there by similar gravels, but not so fine and sandy.
Well-sections throughout Holderness also show the Boulder-clay to

Section at Paull Cliff, near Hull.

N.
Soil and gravel.
Yellow sand.

Fine gravel with a ‘3:5
few shells.

) Ft.

Yellow sand, with 10
patches of gravel

Grey clay, no bed- 12

ding apparent.

extend inland to Hull and Beverley. As this clay could not be seen
beneath the gravels at Kelsey Hill, I proceeded to examine the
river-side section described by Pr ofessor Phillips at Paull Cliff, a few
miles below Hull. I there found several of the same shells (including
the Cyrena, but in much fewer numbers and more broken) in beds of
sand with but little gravel, reposing upon an irregular surface of grey
clay ; but, this clay containing no boulders or fossils, I could not feel
certain about its being the Boulder-clay.

As I could not remain to superintend a series of trenches and
borings which seemed necessary to settle the question of superposi-
tion, my friend Mr. T. J. Smith, F.G.S., of Hull, who had accompanied
me on my last visit to Kelsey Hill and also to Paull Cliff, undertook
to see them carried out; and I am indebted to his active co-operation
for the following results. The difficulties, however, were greater
than we anticipated, and the results less. Owing to the wet season
it was found impossible to dig a trench to any depth at Kelsey Hill;

* The occurrence of the two species of Rissoa has now to be noticed.

>

1861.] PRESTWICH—BOULDER-CLAY, 453

for the line of water-level was reached at a foot or two below the
level of the pit. Boring was then tried, when, owing to the variable
and often very coarse structure of the gravel, the first workmen gave
it up in despair. It was resumed again at a later period with the
obliging assistance of Mr. Monkman, the manager of the Holderness
Line, whose property the pit is. We had hoped to find the base of
the gravel at a depth of 10 to 12 feet; whereas after penetrating
with difficulty to a depth of 36 feet, always in the gravel, but the
lower bed more argillaceous, the work had to be abandoned. These
borings at Kelsey Hill gave :—

Boring at Kelsey Hilt.

eererencine athe Sand and gravel with shells.................. 4 feet
b aus argerioraveluen nesses seeeeeeensa eeeeee 16,
eevee yee licinaller Bravel oo... sees ese se een eee 8

srownaup a> Larger gravel in grey loam (Boulder-clay?) 8 :

36 ,,

I may observe, that although we failed to obtain the desired
exact proof at this spot, yet at places close adjacent, and on the same
level, artesian wells have been sunk which invariably pass through a
greater or lesser mass of Boulder-clay before reaching the water-
bearing beds of sand or the chalk*.

Attention was now turned to Paull Cliff, to ascertain whether or
not the clay exposed at the base of the cliff belongs to the Boulder-
clay. Such proves to be the case; for in digging below the base of
the cliff, Mr. Smith soon found the clay to become stony, and the
specimens he has sent me have the ordinary aspect of the Boulder-
clay.

, Section at Paull Cliff.

Soil and silty gravel.................e00s 8 feet.
Cliff-section, at a short di- | Sand and gravel with shells............ i
stance from the sect. p.452 | Sandy dark-coloured clay without \ 6
GUDMOPhposansooncssdovevadcesoados0G00GH ny

Section obtained by diggi E
=: eae f th a ht “e)) Clay with stones (Boulder-clay).

Looking therefore at all the conditions of the case, I feel satisfied
that these gravels with the Cyrena fluminalis overlie the great mass
of Boulder-clay of Holderness. The question then arises as to whe-
ther these shelly gravels belong to the Boulder-clay, or whether they
are separable from it; and on this point the evidence is not quite
clear, although I am now more inclined than at first to consider it
tolerably conclusive. As observed by Prof. Phillips, there are places
on the coast where patches of sand and gravel are seen intercalated
in the clay, whilst inland the gravels form isolated hills, and the

* At Hull the section of a well given by Professor Phillips shows a clearer
separation of the beds, these being—

Alluvial accumulations .................. 32 feet.
(Bouldexzclavaeencreee eee ec oe sseeeeaese 36 C4,
Sandieete eee er neecronn crane muencean ene PAB). 5,
Chalke er ere aie coe hence W@ sg

TONES

454 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [Apr. 24,

difficulty is at these places to obtain the positive evidence of super-
position. At the pit first mentioned, near Ridgemont, the gravel is
continuous throughout, and no Boulder-clay is seen; but at the
adjacent old pit I found distinct traces of a bed of red clay capping
this gravel, whilst at Kelsey Hill the high face of sand and gravel
at the west end of the pit shows a slight intercalation, near the top,
of a bed, 13 foot thick, of pebbly clay. There is also some higher
ground in the neighbourhood which seems capped by clay.

Section at the west end of the Ballast-pit, Kelsey Hill.
E.

a. Gravel.

6. Clay, with large pebbles.

c. Very coarse gravel.

d. Seams of sand and gravels.

: e€. Fine sands, traversed by
a number of small faults *:
some few shells.

Taking this section in conjunction with the boring, we have here
a thickness of 60 feet of sands and gravels}. This, it is true, is un-
usual on the coast, and it might be asked whether these upper beds
of gravels and sand are not reconstructed out of the clays and gravels
of the Boulder-clay. It has, however, to be observed that in this more
inland portion of the Boulder-clay it would seem that the beds of
eravel and sand are altogether more generally developed—a fact
shown in the two following and other well-sections, for which I am
indebted to Mr. Smith.

* The middle part of the section is so obscured that I could not ascertain
whether the faults proceeded upwards through the beds d to a.
+ The hillock rose in one part (now removed) 56 feet above the marshes.

1861.]

PRESTWICH—BOULDER-CLAY.

455

Section of two Borings* near Hedon, six miles from Hull and about
two miles from Kelsey Hill, (Furnished by the Engineer of the Hull

Waterworks. )
At Old Pollard Farm.

At Twier’s Farm.

Feet Feet.
Sail le cooudonaadsansbsododooHedysouueD600 SOU Eescasnnsts a ansccscebewavacemeste 2
Red brick-clay .........:c...sccsease0 A NaGoodsbrick-cliayi tsv.ccs-sdeecteomevet 5
i leackawarpie cee. sseareesiesee secetsn Oban lackkwarpl seelinttenvaceeenseceutenes 13
Red clay full of stones............... 20 | Strong marly clay with stones ... 40
Rough gravel with sand and spa- | 26 Rough grayel-stones and spa- | 24
TELESO. Js CaS BU Sac SHEA B EBS eines - WAUED ice hore esse cuaasn anaes J
Very fine clay, clear of stones ...... fe) | Isa) (CIE? odoncosebapsandupooopusog sone 1
ABeduotetinities ccarnes-ckacsteessceissenses 2 | Dark-green sand .............0.c0000- 11
Black Moor, decayed wood ......... 2 | Blue clay with white sand......... 2
Blue clay with white sand ......... 1 | Hard mixture of blue clay and| jo
Blue clay with white marl ........° 8 AONE) WEIL”, SoatenocesobonobcoddD a
White marl-clay with small pail g | Red clay with white marl......... 10
blestand|fintaic sieesce Jieestens Chalk ear Gr eekas. ates Aitoele 7
Chalk with bed of sand ............ 5 | White sand which blew up ae 1
Challecleamionfints iiracnesha.csnet 69 the pipes 20 feet high.........
{99 | Chalk clear of flints ............0.. . 504
1784

Here beds of gravel occur low down in the Boulder-clay. The
upper three beds belong probably to the alluvial deposit of the
marshes. The stony clay beneath representing the Boulder-clay,
would, if continued on the same level, range under the Kelsey Hill
sands and gravels, which therefore, so far as superposition is con-
cerned, might form an upper member of this series. But the gravel
is more worn and more shingly than is usual in the mass of Boulder-
clay. It has more the character of beach-shingle; for not only have
we littoral shells, but rounded blocks of chalk, pierced by Annelids
and the Pholas crispata, are also common. These are features which
I did not notice in the coast-section; nor have I there observed,
in those thick beds of sand, the fine lamination and large oblique
bedding. These may be owing to the nearer proximity to the mouth
of the old river. Further, I found in the coarse gravel of Kelsey
Hill pebbles of limestone showing glacial scratches more or less
obliterated. These facts therefore afford grounds to view the Kelsey
Hill gravels as partly reconstructed beds, deriving some of their ma-
terials from the lower beds of the Boulder-clay and associated gravels.
The worn and irregular state of the surface of the Boulder-clay at
Paul Cliff also gives some support to this partial denudation of the
lower beds of the Boulder-clay before the end of that glacial period.
On the coast the gravel-beds associated with the Boulder-clay are
spread out with more regularity and conformability.

The greater number of shells now obtained from these beds show,
however, a more northern character than was at first apparent, and
tend therefore, taken in conjunction with the occasional capping of
their seams of clay like a Boulder-clay, and the fact of a general

* The terms used by the workmen in these and the other well-sections are re-
tained. The small diameter of the bore-hole, and the presence of water, often
vender it difficult to judge accurately of the materials.

456 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,

development of gravels to the westward, to incline me to believe that
these beds are to be referred to the upper part of the Boulder-clay.
The shells are all of recent species, and 33 out of the 40 are still
found on the Yorkshire coast. Nevertheless the presence of such
species as the Natica clausa, N. Grenlandica, Trophon Gunneri, T.
scalariforme, Mangelia pyramidalis, and Littorina squalida, which
have a wide northern and Arctic range, indicates colder conditions
than those now prevailing on these shores, and more in accordance
with what we know of the fauna of this portion of the Post-plio-
cene series.

I have extended this communication to greater length than I in-
tended, my object having been to make known a very remarkable
locality well deserving of further research, and which has an im-
portant bearing upon some questions still under discussion. I reserve
the more theoretical questions connected with the origin and cor-
relation of the strata to a future more general inquiry.

P.S. I annex a series of sections sent me by Mr. Smith, of borings
along the line of railway from Hull to the sea at Withernsea, and
passing through Kelsey Hill, which is situated between Sections
3 and 4.

Sections at the stations along the Holderness Railway.

1. Marfleet, 24 miles from Hull. | 5. Ottringham, 11 miles where the Ot-
Feet. tringham road crosses the railway.
Warne icceatnaso st uaaaaeaeanehteess 30 | Feet.
Salt water sprang from “rotten | Bored! through”. -....sc0--0sa-eaeneee 30
stuff.” Strong marl with stones; not

finding water, was given up.

2. Hedon Station, 524 miles from Hull. |
IBrIO CLAY: ccs s0c'ssachiseg as anecrasnas sae 6 | 6. Winestead Gate-house, 134 miles.
Grey mar] with stones ............... 24 Warp) ares 2.cidevasSscotten eas eee 30
On to abed of sand from which Strong red! marl 7.55. c10seee scenes 5
water sprang. Marl with stones ...........c.sse-e++- 30
3. Burstwick Station, 73 miles from Dirty sand containing water.
Brick ol Hull. ial 7. Patrington Station, 14 miles.
Ce Dp ae sor oso2 se nena ches eanotes on il, Sitons red masl 7... :ssce cco 30
Strong marl with “ iron-stone 29 | 5 3
Strong marl with stones 40 Grey marl with stones ............... 15
= EUdairas Rak ok ae he Sand with water.

Red sand giving sufficient water.

4, Keyingham Station, 9% miles from 8. Withernsea Station.

Hull. Claivsmarl gehen. sac -pin-anponer ae aeenee 15

NEP OD MGA cn nane ier <eaemne sommes 12 | Gravel and sand ...............--005, 5
Marl with BEOUON', ea rencecna sions uate 3 | Strong marl with stones ............ 60
Sand-bed with sufficient quantity Grey sand.and shells) jo7--cessesperee 2

of water. Found water.

At the railway-stations, only small supplies of water are required.

Geol Vol. XVIL_ PL, XIV

Sections, dtial & Mypothetical, of the Coatbrook-date Coalfield. By Marcus WW Scott, sg! F.GS. Vining Tnginect, Se.

vonri
| 3 Section

i— ie

D. MAP OF A PART OF

THE COALBROOKM=DALE COAL-FIELD, a
shewing the Line of Section, the Direction of the Fanls;

the Limits of the Coal-beds Se.

(The finely dotted line indicates the boundary of the Matinstee

and Stirchlee Royalties. |

Seclfon VW.

Ak

1861. | SCOTT—-SYMON FAULT. 457

2. On the “Symon Favurr” in the CoALBRoOK-DALE COALFIELD.
By Marcus W. T. Scorr, Esq., F.G.S., Mining Surveyor, &c.
[Puate XIV.]

THIs paper comprises observations on a section through a part of
the Shropshire Coalfield in nearly a straight line from north to
south—commencing at the Greyhound Pit, near the Oakengates
Tunnel of the Shrewsbury and Birmingham Railway, and terminating
at John Anstice & Co.’s Halesfield Pits near Madeley ; butit is more
particularly intended to explain the nature of the “Great Kast
Fault,” or “Symon Fault,” as it is locally called.

The district of which the section forms a part has been explored
and brought before this Society in a paper “On the Geology of
Coalbrook Dale,” by Mr. Prestwich, published in the ‘ Transactions
of the Society,’ 2nd ser. vol. v. part 3, which fully treats also upon
the fossil fauna and flora. My object is therefore not to enter into
detail further than is necessary to explain the true nature of the
“Symon fault,” alluded to and described by Mr. Prestwich (loc. cit.
p. 432) as far as the data then obtained would allow.

In May, 1843, I commenced my labours in the district, as check-
viewer and surveyor for the owner of the Malinslee and Stirchlee
Royalties, extending over an area of upwards of 1200 acres (within
the dotted line on the Map D, Pl. XIV.). Since 1843 I have made
half-yearly surveys and plans of the workings in the coals and iron-
stones, and have had opportunities of obtaining details necessary for
my object.

The coals (where the whole of them occur) are, in a descending
series, in the property referred to—

In.

6 thick.

ft. in.
ime ther Rop: Coals ach wi. . een bes from 4 0 to
2. The Half-yard Coal ..........
ele Donple;Coaleee = sree er 5
5 ding Neneh Con Fee Sova omic cio 2
melhesbisehlintsCoalk an ater ; 3
pelheiStimkinesCoale no. eee 3
pine ClunchCoalee. i). sant
. The Two-feet and Best (separated
DY MIKCHClAy Ne (cee cers ee
9. The Randle and Clod Coal......
10} The Wattle Klimt Coal. 3.72. .%:

OO NT Od Or OO
SOE S
Dow NWOFEWOaH BS
Wor CODDOD

ase

0
6

the united thickness being somewhere about an average of 33 feet.
The whole have been and are being worked more or less, with the
exception of the Half-yard and Clunch Coal; the Half-yard Coal has
been worked in a small freehold near Oakengates Tunnel on the
Shrewsbury and Birmingham Railway, and there can be no doubt
that ultimately, when the other and more profitable coals are
exhausted, the two exceptions will be worked. In some parts of
the royalty named, another coal, above the Top Coal, called the
Fungus Coal, has been found, but not extending over a large area.

458 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,

The Randle and Clod Coals have been the principal coals used in
the blast-furnaces for making pig-iron—almost exclusively until
within the last fifteen years, when the Little Flint Coal has been
brought into use, and proves to be the best iron-making coal, used in
a raw state,—producing, as I am informed, more iron per furnace per
week than the Randle and Clod Coals from equal weights of materials.
The other coals are mostly used for domestic, malting, and mill and
forge purposes ; but the Two-feet and Best, Big Flint and Yard Coal
are now used partly in the furnaces in the shape of coke. The
Stinking Coal (containing a great deal of sulphur, as its name im-
plies) is principally used by the workmen, for brick-burning, and to
a great extent at the blast-engine, rolling-mill-engine and other
engines for the boiler-fires.

The ironstones of a workable nature, per sé, are, in a descending
serles,—

5 saber } both lying between the Yard and Big Flint Coals.

3. Pennystone, lying immediately above the Stinking Coal.

Above the Top Coal lies the Ballstone (ironstone) Clod, and above
the Yard Coal lies the Yellowstone (ironstone) Clod ; they are worked
or got as far as possible, when the coals are got from below them.

There are other chance ironstones found in the rocks and clods
associated with some of the coals, but it is not necessary to notice
them here. The object in detailing the coals and stones, so far, is
because they bear upon the subject more immediately to be brought
under notice.

When I first visited the locality (May 1843) the Randle and Clod
Coals were being worked at a point near Mount Pleasant (on Map D).
one mile south-east of Malinslee Hall; and on my next visit (Sept.
1843) the workings at that point had been given up, haying been,
as stated, cut off by the Symon fault; but I was subsequently in-
formed by the bailiff who superimtended the workings in that part
of the field “‘ that there was good coal left.” The real cause of stopping
the workings there was, as far as [have been able to learn, the approach
to other property, and the Randle Coal being partly denuded by the
Symon fault, and the great distance (in the Shropshire Coalfield
then considered so) from the shafts. Since 1843 there have been no
workings in the Randle and Clod Coals (the lowest workable coal but
one) near the line of the so-called “Symon fault.” In March 1845
I surveyed the workings in the Top Coal (the highest workable coal)
near Malinslee Hall, up to the Symon fault and adjoining the great
slip-fault, known as the ‘“ Lightmoor fault.” On approaching the
said Symon fault, the coal becomes interspersed with vertical fissures
filled with white marl, from an inch up to nine inches or more in
width; then the marl becomes gradually and completely mixed up
withthe coal until the coal becomes finally tailed out (something as
shown in the sketch on A*¥ s, Pl. XTYV.).

Finding the Top Coal cut off at such a great distance from the
point where the Randle and Clod Coal is stated to have been cut off
(nearly a mile to the south-east), and the vertical depth from the

1861. | SCOTT—SYMON FAULT. 459

top of the Top Coal to the bottom of the Clod Coal being 150 feet,
I concluded that the Symon fault was a gradually denuded surface
of the coal-seams and intervening strata, assuming that the coal-
seams were originally deposited in a horizontal position or nearly so
(this was before I had seen Mr. Prestwich’s paper and sections).

To show the matter more clearly to myself, I obtained from time
to time (through the kindness of the bailiff who had superintended
the sinking of several of the pits in the Malinslee and Stirchlee pro-
perty) the detail of the strata sunk through in five of these pits
(6, c, d, e, & f on the section and map), being nearly ina straight line,
nearly true north and south. I constructed the Section A, having
previously ascertained, by levelling, the relative heights of the
several pit-mouths above the top-water in the Shrewsbury Canal at
the entrance to the Stirchlee Tunnel (the canal is now converted into a
railway), allowing for the height of the pit-mounds as near as I could.

The main faults (Section A) are shown from their generally known
throw or vertical displacement and the depths of the pits combined
(there are a great many minor faults up anddown, which are not shown
on the section) ; from the depths of the pits the “ dip” or inclination
of the strata is also derived.

In 1856 having occasion to report on some property near Madeley,
and immediately adjoining the Stirchlee Royalty on the south, I
obtained a detail of the strata sunk through at Halesfield Pits, near
Madeley, which pits happened to be, according to the Ordnance-map,
nearly on the same straight line (continued from e through f). The
Halesfield Pit is marked g on the section and map, and, from the
information I received at the time, I constructed that part of the
section northwards to the Limestone-fault (j on section and map).
Between the Limestone-fault and a little south of pit fis at present
unexplored ; but should the Limestone-fault have the upthrow north-
wards of 70 yards, as I have been informed, there must be another
downthrow fault southwards somewhere in the blank or unexplored
part. The Section A shows three main faults, which run nearly
parallel to each other from south-west to north-east (as shown on
Map D). The first, in Stirchlee Royalty, a little north or left of
pit ¢, has an upthrow north of 50 yards; the second, a little to the
left or north of pit 6 (the Lightmoor fault), has an upthrow north
of 130 yards. In 1858, having to report on the minerals under the
Oakengates Tunnel of the Shrewsbury and Birmingham Railway, I
obtained the depths (to the coals only) from the surface, and the level
of the pit above the canal-water, at a pit close upon the tunnel,
called the Greyhound Pit, which according to the Ordnance-map is on
a straight line north with the pits ¢ and 6 in Malinslee Royalty.

The position of the Greyhound Pit is marked a on the Section A
and Map D. A little to the north of the pit @ is the third main
fault, having an upthrow north of 30 yards; I show these coals
with a less dip than the other parts of the section, but without any
very positive data to determine the same. The fault near to pit g
(7 on Map D and Sections A & B) is a cross fault running from north-
west to south-east, and has a downthrow north of 30 yards; the

460 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [Apr. 24,

Limestone-fault runs nearly due east, and has an upthrow north (as
stated) of 70 yards. The other faults shown on Section A are mostly
cross faults, running between the main faults; that at 7 on Section
A and Map D having a rise N.W. of 11 yards, and m a downthrow
north of 30 yards. The Section A is on a scale of 12 chains, or 792
feet to an inch horizontal, and 200 feet to an inch vertical.

There is, except in some few instances, scarcely any perceptible
dip of the strata, as in working the minerals the horse-roads are
driven in all directions; still the general dip appears to be from
south-west to north-east. The Section A, by the depths of the pits,
shows the dip from south to north at an angle of 2° 28’, or 1 in 25.

Looking at the Section A, it conveys but a very indistinct notion
of the denudation or Symon fault, im consequence of the dip and
the slip-faults. It therefore occurred to me that it would not be
an unwarrantable geological liberty to assume that the coal-beds
were originally deposited in a horizontal position, or nearly so; and
that the true nature of the denudation or Symon fault might be
more clearly shown by plotting the*several sinkings upwards, taking
the Little Flint or lowest workable coal asabase. Such is shown in
Section B. The dark line at the top corresponds with the present
surface-line on Section A (without reterence to the dip of the strata on
Section A). That part of the Section B, from point E, about 180
yards south of pit f, to pit 6, on the north, shows the denudation
(or cutting off of the coals and several strata above) up to what is
locally called the ‘‘Calamincar,” as actually proved by the sinkings,—
the Top Coal being cut off at a point about 2100 yards north of pit f,
the Double Coal (28 feet below the Top Coal) at about 1100 yards,
the Yard Coal (8 feet below the Double Coal) at about 770 yards,
the Big Flint Coal (25 ft. 9 in. below the Yard Coal) at about 440
yards—all north of pit f,—and the Stinking Coal (47 feet below the
Big Flint Coal) close to pit f; from point F, Section B, to pit g
may also be taken as proved. Between E and F, a distance of
about 1300 yards is assumed (on Section B), and I think may be
fairly so, when we take into consideration the identity of the strata
at pits fandg. The present depths of the pits to the Little Flint
Coal are as follows (some of the pits are not sunk to the Little Flint
Coal, but the distance below the Clod Coal is pretty uniform) :—
at pit 6, 751 ft. 9in., in which the Top Coal and all the coals below
are found; at pit c, 669 ft. 1 in., and pit d, 492 ft. 9in.; in these
two pits the Top Coal is absent, but all the other coals are in.
Pit eis 593 ft. 1in.; but here the Top, Half-yard, Double, and Yard
Coals are absent, the others below being in. Pit fis 489 ft., but the
Top, Half-yard, Double, Yard, Big Flint, and Stinking Coals are
absent. Pit g is 836 ft.10 in., with all the coals in, but more
divided than at pit 6; the two detached sections at C, 60 feet
to an inch, show from the top of the Top Coal to the bottom of
the Little Flint Coal; that on the left (p) being at pit b, and that
on the right (g) at pit g; im the space (7) between are shown
the connexion and subdivision of the strata: pits 6 and g are
4484 yards apart. The top of the Top Coal at pit g is at present

1861. ] SCOTT—SYMON FAULT. 461

somewhere about 147 ft. 6in. below the top of the same coal at
pit 6. From the top of the Top Coal to the bottom of the Yard Coal
(including four coals, 14 ft. 9 in. thick) at pit bis 40 ft. 9in., whilst
at pit g it is only 11 ft. 7in., and the four coals are only 9 ft. 4 in.
thick ; the Half-yard, Double and Yard Coals being respectively
1 ft.6in., 1 ft. 8in., and 1 ft. 8in., which at pit 6 are 1 ft. 6in.,
6ft., and 2ft.9in. From the bottom of the Yard Coal to the bottom
of the Big Flint at pit 6 is 25 ft. 9in., whilst at pit g the distance
is 89 ft.; there is actually no Big Flint Coal in pit g, but it is found
close to on the north of the pit; there is also no Blue Flat nor White
Flat Ironstone of consequence at pit g. From the bottom of the
Big Flint Coal to the bottom of the Stinking Coal (4 feet thick) at
pit 6 is 47 ft., the Pennystone Clod above the Stinking Coal
being 20 feet thick. At pit g the distance between the two coals is
only 19 ft.6 in.,— the Stinking Coal being only 1 foot, and the Penny-
stone Clod 5 feet thick. From the bottom of the Stinking Coal to
the top of the Clunch Coal at pit is 27 feet, and at pit g it is
18 ft. 6in., the space between being called the Clunches. From
the top of the Clunch Coal to the bottom of the Clod Coal at pit 6
(five coals, 9 ft. 6 in. thick) is 13 ft. 6in., and at pit g (eight coals,
12 ft. 5in. thick) it is 39 ft.. From the bottom of the Clod Coal
at pit g, to the bottom of the Little Flint Coal (1 ft. 6in. thick) is
13 ft. 6in., and at pit g it is 21 ft. 6 in., the Little Flint Coal being
2ft. 3in. thick. The total depth from the top of the Top Coal to
the bottom of the Little Flint Coal at pit bis 167 ft. 6in., and at
pit g 198 ft. 7in., or 31 ft. lin. more. The total thickness of coal
at pit 6 is 82 ft. 9in., of which 29 ft. 3 in. is worked at present, and
the remainder will no doubt be worked at some future period. At
pit g, the united thickness of coal is 29 ft. 9in., of which 19 ft. 7in.
may be taken as workable, the other seams being too thin to be ever
worked profitably.

The first stratum or measure above the Top Coal, which is per-
sistent throughout the several sinkings, is locally called the “ Cala-
minear”’ (No. 12 on Sections A & B). It is found in all the pits (in
pit d merely a trace), and is of a variable thickness from 1 to 153 feet ;
it is of a mixed red, blue, and yellow colour. At pit Z’ it is 33 feet
thick, pit Z'’ 48 ft. thick; pit 2’! 22 ft., and pit 2’ 16 ft. 6 in.
From the bottom of the Calamincar to the top of the Top Coal at
pit b is 92 ft. 6 in., and at pit g 59 ft. At pit f the Calamincar rests
upon the flint rock, which is 62 feet below the Top Coal at pit 6,
and 94 ft. 9in. at pit g (difference 32 ft. 9in.); from the bottom of
the Calamincar to the bottom of the Little Flint Coal at pit 6 is
260 ft., and at pit g 256 ft. 11 in. (difference 3 ft. lin.) The strata
between the Calamincar and Top Coal at pit 6 gradually diminish
southwards till at pit e none of them are found; neither are any of
the coals and intervening strata from the Top Coal to the bottom of
the Yard Coal in that pit, the Calamincar resting upon the top of the
Blue-flat Ironstone-clod. At pit d the Half-yard Coal is represented
by “‘slummy or slaty measures” 2 ft. 6 in. thick, the Top Coal
being denuded or cut off by the Symon fault between pits 6 and c,

VOL, XVII.—PART I. 21

462 PROCEEDINGS OF THE GEOLOGICAL society. _[ April 24,

and the Double and Yard Coals between the pits d and e. It would
appear that a surface at one time existed, rising from the top of the
Double Coal Rock (which occupies the space between the Double
Coal and Half-yard Coal, above) at pit d to the top of the Ballstone
- Clod (above the Top Coal) at pit 6 at an inclination of about 1 in 50,
or an angle of 1°15’, and that the strata from the Ballstone Clod up
to the Calamincar were subsequently deposited on that surface, and
which were again partially washed away down to the Flint-rock at
pit f, on which the Calamincar rests, the Flint-rock resting upon
the Upper Clunches—the Stinking Coal and Pennystone-measures
having been denuded previous to the deposition of the Flint-rock, as
shown by the small depression in the section. Above the Calamincar
comes the Rough Rock, very uneven in the bottom and irregular in
thickness (15 to 51 ft.; average 28 ft. 9in.); and in many places
it is a complete conglomerate. Above the Rough Rock comes the
«« Brickman’s Measure,” brickmaking-clay 6 to 15 ft. thick. Imme-
diately above the Brickman’s Measure there are two clods or clunches,
together from 5 to 15 feet thick, including two coals in some of the
sinkings, 1 foot thick each. Above these clunches come “strong
binds,” and rock of variable thickness (72 ft. at pit 6, 80 ft. at pit ¢,
78 ft. 6 in. at pit d, 67 ft. 6in. at pite, 29 ft. at pit f, and 97 ft. 4 in.
at pit g) up to two coals which occur in all the sinkings, 1 foot thick,
with fire-clay between and clod below, from 3 ft. 6 in. to 8 ft. 9 in.
thick together. Immediately above these small coals is the Stinking
Rock, varying from 49 ft. to 61 ft. 6in. in thickness—average
52 ft. 6in.; it is at this rock that the water is coffered or tubbed
back throughout the district. Above the Stinking Rock there are
clunches and rock-binds from 48 ft. to 84 ft. 6 in. thick—average
69 ft. At pit g two coals occur in the same, 6 inches and 3 inches
thick respectively. In some of the sinkings these clunches are
divided into many parts—in others they are not divided. Above
these clunches comes a rock, called the Thick Rock. It is described
as “rock” in all the sinkings, except pit c, where there is 20 feet of
“dark sticky shades and clod;” it is 51 feet at pit 6, and gradually
thickens up to 90 ft. 4in. at pit g—average 67 ft. 8in. Above the
Thick Rock come clunches and clods 45-81 feet thick—average,
58 ft. 3inches; at pit g, 18 ft. above the Thick Rock there is a coal
8 inches thick. Next above these clunches comes the Top Rock,
described as rock in all the sinkings where it occurs, but pit 6; it
is 27 ft. at pit g, 24 ft. at pit f, 27 ft. at pit e; it is not in pit d; it
is 57 ft. thick at pit c, and at pit b 24 ft. of rock, but 57 feet,
including 33 ft. of red clunch, white clod, and brown clunch. It
is quite possible that close attention has not been paid by the sinkers
to the divisions in pit c, and that a stratum of clod and clunches
exists in that pit not taken notice of, seeing the uniformity of the
rock itself in pits b,e, f,andg. Above the Top Rock at pit g there is
3 ft. of blue clunch, and above that 135 feet of red clay; at pit f
there is 15 ft. of clay and earth; at pit e 49 ft. of blue and red clay
above the Top Rock, and at pit 533 feet of blue and red clod and
elunches with a chance-coal 1 ft. thick. I have not been able to get

1861.] SCOTT—SYMON FAULT. 463

any specimens from the strata above the Calamincar to determine
the era, &c.* ; but from the appearance of the rocks exposed to view,
and the many coals interspersed, they appear to me to belong to the
true coal-measures ; on the Geological Survey Map they are coloured
as belonging to the coal-measures. The Sections A and B are on too
small a vertical scale to show at the several pits in detail the several
divisions as given by the sinkers. At pit 6, from the surface to the
bottom of the Little Flint Coal there are 68 divisions, and at pit g
89 divisions.

The table on pp. 464, 465 shows the depths from the present sur-
face to, and the thickness of, the main measures (the clunches not in
detail) at pits 6, ¢, d, e, f, and g.

From a general review of all the circumstances, there can be no
doubt that the Great Symon fault, as shown by Section B, and
proved by actual facts to the north of pit f, indicates the existence
of an old valley or estuary of denudation of the coal- and ironstone-
measures, In which subsequently other strata of the coal-measures
were deposited; and that these were partially washed away again.
The deepest part of this old valley appears to me to be somewhere
about pit f, where the coal-measures have been washed away as deep
as the Upper Clunches below the Stinking Coal, and where the Flint-
rock rests immediately upon the Upper Clunches, which occur in all
the sinkings, and varies from 13 to 27 feet thick—the average being
21 ft. 7in. The information that I have been able to obtain as regards
the Randle and Clod Coal south of pit f leads me to the conclusion
that the Symon fault has never entirely cut off that coal and the
three coals immediately above; and that the working of the Randle
and Clod Coai in a southward direction was given up partly in conse-
quence of the coal beimg a little deteriorated by the denudation,
partly from the inflammable gas being more abundant, and from
there being plenty of coal northwards of pit f to work, and less
faulty: besides, to work further south would require more sinkings,
whilst there were plenty of pits to obtain the said coal (then consi-
dered the best furnace-coal) to supply the furnaces which were at
that time at the extreme north end of the éstate with which I am
more particularly acquainted; and as we find the whole of the coals
at pit g but slightly altered as to their relative position and thickness,
with the Calamincar and the several rocks and clods above (which
there can be no difficulty in identifying with the strata sunk through
at the other pits), there is every reason to suppose that the coals
come in again southwards of pit f, something in the manner repre-
sented in Section B, but of course altered by the dislocations and the
dip. Assuming such to be the case, there is every probability of
an area of coal and ironstone being found (at least it is to be hoped
so) at a workable depth in the district, and possibly underneath
the Lower New Red Sandstone, where hitherto none was ex-
pected by the practical workers. I express this opinion from the

* Mr. Prestwich has treated of the strata and their fossils fully in his memoir
above cited, pp. 444446, &e.
212

[April 24,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

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466 PROCEEDINGS OF THE GEOLOGICAL socleTy. [April 24,

circumstances detailed above, and shall be glad if it should meet
with the support of those gentlemen of the Society who have given
more attention to geology than myself, and are consequently much
more able to explain their views and advance hypotheses more in
accordance with nature’s laws: the subject is of vast importance,
national and individual.

On the Map D I have attempted to lay down by dotted lines
(t—y) the general line of denudation of the several coals, &c.
on the north side of the old valley or estuary, as derived from my
surveys and the sinkings in the Malinslee and Stirchlee Royalties,
and from the sinkings in other fields.. At the Castle Pits near
Great Dawley Church, the Top and Half-yard Coals are absent, the
Double and all the other coals, &c. bemg in; at the Mill Pit, a little
further to the south, the Top, Half-yard, Double, Yard, and Big
Flint Coals are absent, the Pennystone and all the measures below
being in.

About half a mile north-west of pit ba pit has been lately sunk,
30 yards below the Little Flint Coal, of which the following is the
detail, measured by myself Oct. 5, 1857.

_ Total depth below L. F.

yds. ft. in. yds. ft. in
| Be Tn GY CN ees Se iO Og 10s 26 10) «226
OR ATID Gy. bi MRE IUNS ts was Os OP Oes6 LE Ovo
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Si Rock andspmds. .. 4. see. 1b 220
9. Hard Bastard Rock with
rough pebbles. (Left af 7 Pa) 30 0 0

SIBEIMO ic beds ahchae a ss

REFERENCE TO ILLUSTRATIONS IN PLATE XIV.

A. Section of the strata as they at present’
GIT |Bedgueche at oddboosooRob spon anbaascaino=

B. Section of the same strata as in A,
plotted upwards from the Little Flint
Coal as an assumed base ...............

Horizontal scale, 12 chains=1 inch:
and vertical scale, 200 feet=1 inch.

€. Enlarged comparative sections of coal-
seams at pits band g.............--..-...

D. Map showing the line of section, &.... Scale 1 nch=a mile.

Sections A, B, and C.
a. The Greyhound pit near Oakengates Tunnel.
b. Pudley Hill Pit, Malinslee and Stirchlee Royalties.
c. Lawn Pit =
d. Wharf Pit -
e. Cook’s (or Cuxey’s) Wood Pit
f. Grange Pit
g. Halesfield Pits, near Madeley.

} Scale, 60 feet to an inch vertical.

”?

1861. ] SCOTT—SYMON FAULT, 467

h, Level of top-water of the Shrewsbury Canal at entrance to Stirchlee
Tunnel as it existed previous to being converted into a railway.
hk’. Present surface-line.

z. Fault, downthrow north 30 yards.
j. Fault, said to have an upthrow north of 70 yards.
[os 2 ae ‘upthrow north of 00 yards.
UB Seas 11 yards.
ee stp down-throw north of 30 yards.
nm. ,, upthrow north of 130 yards.
30 yards.
- Enlarged section from Top to Little Flint Coal at pit 0.

q: at pit g.
Tr. Space between the two pits 4484 yar rds.

A* s, Sketch showing the Top Coal in connection with the Symon Fault.
Map D.
¢. Line of denudation of the Top Coal.

- 3; Double Coal.
Fo 5 Yard Coal.
Big Flint Coal.
53 Stinking Coal.
» partial denudation of the Randle Coal.
Z. Western limit of Lower New Red Sandstone—Geological Survey.
Z'. Forge Meadow Pit—Calamincar 33 ft. thick.

Z''. Wood Pits 4 48 ,,
Z'". Spout Pits is DPN i ee
Z''" Randley Pit 3 16 ft. 6 in.

Z°, Railroads.
Sections A & B.

1’. Red clay. 17. Half-yard coal.
1. Blue and red clod and clunches 18. Double coal rock.
with a coal at pit 0. 19. DovusuE coat.
2. Top rock. 20. Yellowstone (ironstone) clod.
3. Clunches and clods. 21. Yarp COAL.
4, Thick rock. 22. Blue-flat ironstone clod.
5. Clunches and rock-binds. 23. Pitch of basses (rock at pit 7).
6. Stinking rock. 24, White-flat ironstone clod.
7. Fire-clay clod and coals. 25. Bia FLINT COAL.
8. Stony binds and rock. 26. Flint-rock.
9. Clunches, with coals. 27. Pennystone (ironstone) clod.
10. Brickman’s measure. 28. STINKING COAL.
11. Rough rock. 29. Clunches (fire-clay).
12. Catamincar (the first persistent 30. CLUNCH COAL.
stratum above the principal 30'. Two-FEET COAL.
coal-seams). 30", Bust Coat.
13. Rock-binds and clod. 30!", RANDLE and CLOD COAL.
14. Ballstone (ironstone) clod. 31. Clunch and hard rock.
15. Top coal. 32. LirrLe FLINT COAL.

16. Bass and slaty measure.

May 8, 1861.

Robert Mills, Esq., F.S.A., Rochdale; Edmund William Ashbee,
Esq., 14 Rutland Street, "Mornington Crescent; and Captain
Willoughby Osborn, C.B., Madras Army, were elected Fellows.

The following communications were read :—

468 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 8,

1. On Two Bonz-caverns in the Montaene pu Ker at Massa, in the
Department of the Anikce*. By M. Atrrep Fonvan.

(Communicated by M. Lartet, Foreign Memb. Geol. Soc.)
[ Abstract. |

Tux Valley of Massat, situated near the centre of the Pyrenees,
opens to the west between two lofty mountains, which, at first
approaching each other, spread out and diverge as they extend on
the south-east towards the mountain-range of which they are the
ramifications, so that in this direction the valley has no outlet. It
thus forms an elongated basin, of a triangular form, the base of
which extends along the side of one of the great spurs of the Pyre-
nees (see fig. 1), whilst the apex forms a narrow and winding gorge
which affords the only outlet for the waters of the valley.

A short distance above the spot where the basin commences, namely
on the western side, near the apex of the triangle, a high mountain
of limestone rises up, which, advancing abruptly into the valley, forms
an elevated promontory, against which the torrents or diluvial waters,
which appear to have inundated this region at one or several remote
periods, must have rushed. It stretches out almost at a right angle
from the southern side of the basin; and, exactly where it extends
furthest into the basin, its crest forms a mound or hillock, the
summit of which is considerably more elevated than all the sur-
rounding heights. The whole of this mountain, which has been
violently disturbed and disjointed, is bare, and is filled with fissures,
crevices, and deep hollows or grottos, the principal galleries of which
extend from N.N.W. to 8.8.E., parallel to the longitudinal axis of the
valley.

Amongst these caves two are remarkable on account of their
extent.

One of them, situated near the summit of the mount, at an ele-
vation of about 100 metres (330 feet) above the bed of the valley, is
approached by a spacious vestibule, or outer chamber, with two large
and lofty circular entrances, one of which faces the north, the other
N.N.W. (see figs. 1 & 2). The soil of the outer chamber, which,
like the rest, was devoid of all stalagmitic concretions, was smooth
and horizontal, rising above the sill of the entrance. With the ex-
ception of a small portion near the N.N.W. entrance, where a few
fragments of pottery were found, mixed with cinders and coal, it
presented the appearance of an abandoned river-bed. A sandy loam
sprinkled with gravel or small rolled pebbles occupied the centre ;
whilst at the edges against the wall of rock, larger but similarly rolled
pebbles appeared to have been thrown up by the eddying or movement
of the water. These deposits continued in the same way for a di-
stance of a hundred metres along the principal gallery, only dimi-
nishing in thickness as they extended further inwards, and entirely
ceasing at the further end.

This arrangement, combined with the presence, at such a consider-
able elevation, of rolled pebbles, most of which were different from

* A brief notice of this subject is given in the Quart. Journ. Geol. Soc.
vol. xvi. p. 491.

470 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 8,

Fig. 2.— View (from the north-west) of the Montagne du Ker,
showing the entrances of the Upper and the Lower Caverns.

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3 iS Sy fintone bt be AN
\ BS. \ a ‘ 4
\ a Ze ANI Hey
1 ay Vn Sy a ae) oat ‘
Mh ek
t= ee : (“7
Sy ry { SS ee SIS GD 6% 1 ae aN
CA pes zs Ro = ~ iF ‘fx y we
Aye { c4 L Sar ee Ee» | (Gees oe
i] Bak Ta Ore. i S\ SO
WL ee. \o ok ; a) \ 26
N <- 4A SS. Cy % ee
i One = 7
wo \ UES we ae a =
= 4 Ho an S ~ oN
= ag — yr ? Ra = >
SS SS ~

the rocks of which the mountain consists, appeared to the author as
solely attributable to those diluvial cataclysms which geology points
to as haying occurred at several periods anterior to historical tradition.
In order to understand these facts, he determined to study the nature
of the deposits ; for which purpose he caused a deep trench to be
dug in the soil near the northern opening, and extended it to the
lateral walls. The result of this first attempt was the discovery of
a large quantity of bones of Carnivora, Ruminantia, and Rodentia,
amongst which were most abundant the great Cave-bear described
by Cuyier, a large species of Hyena (H. spelea), and a large Felis
(tiger or lion), all mixed together, rubbed, and broken, giving evi-
dence of a distant transport, or at least of a viclent displacement.
Besides the cinders and charcoal at the surface (with which were
associated fragments of pottery, an iron poignard, and two Roman
coins), another bed of cinders and charcoal was found at a depth of
more than three feet in the ossiferous loam, and here M. Fontan
found a bone arrow-head and two human teeth (fig. 3) ; the latter
were at a distance of 5 or 6 metres one from the other.

Fig. 3.—One of the two Human Teeth found in the
Upper Cavern, Montagne du Ker, Languedoc.

The second or lower cavern is situated at the foot of the mountain,
close to the road, at an approximative height of 20 metres above

Fig. 4.—Bone Arrow-head from the Lower Cavern, Montagne du
Ker, Languedoc.

the bed of the river (see figs. 1 & 2). Its only opening (which,

1361.] FONTAN—BONE-CAVERNS OF MASSAT. 471

like those of the upper cavern, is contrary to the present direction of
the water) leads into a tolerably spacious chamber, the ground of
which consists of a blackish earth and of large rolled pebbles (some
of them granitic), amongst which are scattered, in the greatest con-
fusion, fragments of bones belonging to animals either of extinct spe-
cies or of such as have for the most part long since ceased to inhabit
these regions. They belong principally to Deer (Cervus elaphus),
Antelopes, and Aurochs; and there were a few remains of feline
Carnivora (apparently a Lynx). Amongst these were found worked
flints and numerous utensils of bone (deer’s bone chiefly), such as
bodkins and arrows; the latter were the most numerous, and are
carved with oblique grooves, probably for poison (see fig. 4). Some
of the bones bear marks of incisions made by sharp instruments in
flaying or cutting up the carcases.

In each cavern a chasm crosses the gallery and terminates the
deposits ; in the upper cave at 100 metres, in the lower one at about
7 metres from the entrance.

M. Fontan argues that rain-water could not have introduced nor
arranged the deposits within these caverns; and that the position of
the entrances of the caves (facing the N.W.), and the presence of the
fissures which cross the caves, preclude the idea of the waters of any
torrent from the Pyrenees leaving these deposits on the floors of
the caverns. He observes, ‘“‘ From all these phenomena, the most
striking feature in my opinion is this, namely, that the Valley of
Massat appears to have been at one and perhaps at several periods
the theatre of a vast inundation coming from the N.N.W. or West,
in the opposite direction to that of the present course of the waters
Oterhismesions 77 teks cede “The fact of a flood produced by torrents
capable of filling up this valley is not a simple accidental occurrence
to be explained by causes purely local. If it existed, similar effects
must have been produced in all the neighbouring regions, and must
even have extended to a great distance. It would have been a true
deluge, destroying everything on its passage ; and, as history is silent
on the subject, we cannot believe it to have been of recent occurrence.
If then the entombment of human remains under the upper bed of
cinders and charcoal is to be attributed to this. cause, the appearance
of man in these regions would date from a very distant period.”’

“Tn conclusion (says the author) we may deduce from these facts,—
1st, That a diluvial current penetrated into the Valley of Massat,
coming from N.N.W. or West towards the S8.8.E. or East. 2ndly,
That this current did not continue for along time. 3rdly, That Man
and all the other animals the remains of which are buried in these
caves existed in the valley before this cataclysm. 4thly, That the
greater part of these animals inhabited these caves; from whence we
must suppose that Man was not the contemporary of all of them. In
fact we cannot admit that he lived in this narrow valley at the same
time as the Lions, the Hyeenas, and the Bears; we cannot even admit
that all these animals existed there at the same time, either because
they do not usually inhabit the same climate, or because their habits
are incompatible. Hach kind inhabited the cavern successively ; and
Man was probably the last. When he appeared there was probably

472 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 8,

nothing remaining but the Deer and other Ruminants, which would
satisfactorily explain why the tools which have been found were
made exclusively from the bones of these animals.”

List of objects found in the two Caverns above-mentioned, according to

M. Larter.
(@igerforviGionn tain de. ech ayes Fragment of a lower jaw, and

3 or 4 detached teeth.

Daye EN AMS aS RRR, Half of a lower jaw.

intyeenay (ELS pelorm)).ee en ere: Several teeth and ungual pha-
langes.

Bear (Ursus speleus,Cuv.).... A great number of teeth and
various bones.

Badger svi is. 4 5 eee: eee Three fragments of the jaw and

afew detached teeth. (These
remains appear to be more
recent than those of other

5 species. )

SS Ai BUG e OB 36 mooin Hig Jo ac Five or six teeth.

s | Sheep or Antelope .......... Two teeth.

e& | Roebuck .................. Half of a lower jaw.

Ear itDos. tHoxorsyolt. Seok. ae Incisor and molar teeth.
Rodent (Mus sylvaticus) .... Several teeth and fragments of

a jaw.

Water=rat (2. 2 eters Half of a lower jaw.

Hedgehog (Erinaceus europeus) Half of a lower jaw.

Two human teeth and an arrow of bone. (This arrow has
been lost, and M. Lartet has never seen it, so that it is impos-
sible to say whether it was made of the bone of a Ruminant
like those found in the lower cavern (fig. 4), or of the bone of
a Carnivorous animal.)

\ Cinders and Charcoal.

( Bear (probably the existing

Bear of the Pyrenees).... A fragment of a lower jaw.
Tyme ech bark See ae Doe Lower canine tooth.
Cat: (dels caius) 2%, 5. 2eisne Two or three fragments.
Deer (Cervus elaphus)...... Numerous antlers, sawn and

earved bones, all of which
have been intentionally broken,

3 | many jaws, and a few scat-
3 y, tered teeth.

s | Ox (Bison priscus) ........ Half of a lower jaw, and horns.
E Goatiordibex use eenergr. 3c! Meny remains.

4

Sheep or Lesser Moufflon .. A fewbonesand fragmentsof jaws.

Chamois (Antilope rupicapra) Maxillary bones, jaws,and bones;
and a horn showing marks that
the animal was skinned in a
fresh state.

Birds (Magpie and Jay) .... A few rare fragments.

Wald Boar oh) cccoeten set A molar and a few fragments.

_
o's)
fon)
pea

ey

JEFFREYS—CYRENA FLUMINALIS. 473

Remains of Human Industry.

Several bones of Ruminants, chiefly of Cervus, worked up as
arrows and carved with spiral grooves, needles, coins, harpoons,
bodkins, &ce. Two vertebre of a large Fish resembling those of
[se Cod-fish, and fragments of chipped flints. There were also

Lower Cavern.
glee ae

some specimens of white flint chipped into the form resembling
what are called “ knives.”

Note by M. Larter, For. Mem.G. 8.

I regret that M. Fontan has not inserted here, as in one of his
former communications, any notice of the Megaceros Hibernicus *: it
is true that when I recently made some excavations in the lower
cavern of Massat, I did not find the slightest fragment which ap-
peared to belong to this large extinct Ruminant; but, as there was
found amongst the objects formerly collected by M. Fontan, a frag-
ment of a palmated antler referable to the Megaceros Hibermcus, he
would, perhaps, have been of opinion that it should have appeared in
one of these lists. The existence of remains of this fossil Deer has
been proved in other spots at the foot of the Pyrenees, so that there
would be nothing improbable in its occurrence in one or the other of
the caves of Massat. With regard to the Cervus pseudovirginianus
(M. de Serres) mentioned in the former lists+, I have myself sug-
gested its omission, because the distinctive characters which led me
to adopt this species do not now appear to me to be sufficiently made
out, and they depend, if I am not mistaken, on mere varieties of form
attributable to a difference of age or sex.

2. Notes on some Furturr Discoveries of Frint ImpLeMEnts in Beds
of Post-PLIocENE GRAVEL and Cray; with a few Suggestions for
Search elsewhere. By Josrra Prestwicu, Esq., F.R.S., Treas.G.s.

[This paper was printed in the August Number of the Quarterly Journal (p. 362)
by permission of the Council. ]

3. On the Corsicuia (or CyRENA) FLUMINALIS geologically considered.
By J. Gwyn Jurrreys, Esq., F.R.S., F.G.S.

[Abridged.]

Mr. Jerrreys having stated that he had identified the species of

Corbicula found by Mr. Prestwich in a raised sea-beach at Kelsey

Hill¢, in Yorkshire, with that of the Grays deposit, as well as with

the recent species from the Euphrates and the Nile, proceeded to
* See Quart. Journ. Geol. Soc. vol. xvi. p. 492.

t+ Loe. cit.
t See above, page 446.

474 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 8,

give a sketch of the history and synonymy of the species under con-
sideration ; and he added some remarks which follow.

In 1774, O. F. Miller (the celebrated Danish naturalist) described,
in his ‘ Verm. Terr. et Fluv. Hist.’ p. 205, a shell from the River
Euphrates, under the name of Tellina fluminalis. His description
exactly corresponds with the triangular form of the fossil shells from
Kelsey Hill and Grays. In 1811, Megerle v. Mihlfeldt founded on
this and other allied species the genus Corbicula; which name is
now adopted by conchologists. In 1818, Lamarck proposed for the
same species the generic name of Cyrena; apparently not beimg
aware of Muhlfeldt’s publication.

Many recent species of Corbicula (or Cyrena) have been described
by Lamarck, Férussac, and others. The most westerly station given
by any of the conchologists is the Nile. Goldfuss, Nyst, Galeotti,
Philippi, Searles Wood, and others have also described many Tertiary
species of Corbicula (or Cyrena) under other names. The most
easterly locality given by any of the paleontologists is Cefali, near
Catania. It is, however, highly probable that most of these species,
whether recent or fossil, ought to be united.

The tendency to variation in freshwater shellsis very much greater
than in their marine analogues. Almost every river, or piece of stand-
ing water, yields a different form of Anodonta cygnea, or of Limneus
pereger ; and the number of “ species” that have been fabricated out
of these forms is astonishing.

The range of locality or station among freshwater shells is equally
great, and far exceeds that of marine shells. <A species of Physa
which inhabits the West Indies, and called Physa Jamaicensis,
cannot be distinguished from a variety of Physa acuta, a well-known
European species; while species of Limneus, Pisidium, and other
freshwater shells from the East Indies, and even from Siam, so closely
resemble in every respect those of Western Europe, that it is only by
calling them “representative” species that any pretence for distinc-
tion can be maintained*.

Taking, therefore, into consideration the extreme variability and
ubiquity of freshwater shells, it is not surprising that the Corbicula
jluminalis should have at one period inhabited that part of the Kuro-
pean continent which now constitutes Great Britain as well as Sicily
and the valleys of the Euphrates and Nile. Even in the case of
marine shells, nearly one-half of the species which now inhabit the
Mediterranean also exist in our seas, while many other British spe-
cies occur in Sicily in a subfossil state; thus showing that the area
of distribution was once more extensive than it is at present, and
that it has been since limited by climatal or other causes. From
Sicily to the mouths of the Nile the distance is not considerable.

* Since writing the above, I find that at a Meeting of the Zoological Society
of London, held on the 8th of July, 1856, Mr. 8. P. Woodward made a very
interesting and important communication on this subject. In giving a list of
some land and freshwater shells from Kashmir and Tibet, which Dr. T. Thomp-
son had collected in the Himalaya, Mr. Woodward noticed that “one half
were British species, and the rest of the commonest and most widely diffused
Indian forms.”

1861. ] GREGORY—WESTERN AUSTRALIA, 475

Some minor facts in relation to Mr. Prestwich’s discovery may be
worth noticing.

One is, that the beaks of the shells in question are not eroded,
as is generally the case in recent specimens. From this I should
infer that the chemical nature of the water in the ancient river or
estuary inhabited by the Corbicula was different from that of the
water which composes the Euphrates or the Nile.

Another is, that the size of the semi-fossil shells exceeds that of
any recent specimens which I have seen of the same form. This
seems further to exemplify a fact which I have elsewhere noticed ;
namely,that when any species of shell is distributed over a wide area,
having a northern and southern range, northern specimens are larger
than those of the same species from southern localities.

The former existence of the Corbicula in this country does not
warrant any inference that the climate must have been warmer
during that period than it is at present, or that the Corbicula (to
use a vague phrase) “retreated” south after the glacial period. It
more probably was contemporaneous with the Natica clausa and
other shells called “‘ Arctic;”? some of which have survived, while
others have become extinct, in the seas which immediately surround
the British, as well as the Sicilian coasts. A similar inference as to
climate formerly prevailed with respect to the Mammoth. Changes
in the relative distribution or juxtaposition of sea and land, an altera-
tion in the depth of water or in the oceanic currents, an elevation or
depression of the land (especially if it were alternate or sudden),
the absence, diminution, or deterioration of food, the increase of
natural enemies, epidemic diseases, sterility, and many other accidents
(independently of climate and the agency of man), may, in the course
of those unknown ages which succeeded the Tertiary epoch, have
caused the extermination of many species throughout a more or less
extensive area.

May 22, 1861.

Silas Bowkley, Esq., Mining Engineer, Batman’s Hill, near Bil-
ston, Staffordshire; John Edward Forbes, Esq., 3 Faulkner Street,
Manchester; and Captain Francis William Henry Petrie, H.M. 11th
Regiment, Portsmouth, were elected Fellows.

Gustay Bischoff, Professor in the University at Bonn, was elected
a Foreign Member.

The following communications were read:
1. On the Guonocy of a Part of WrstERN AUSTRALIA.
By F. T. Grucory, Esq.
[Communicated by Sir R. I. Murchison, V.P.G.S., &e. &e. &e.]

Introduction.—In presenting to the Geological Society the accom-
panying collection of specimens and this sketch of the geology of a
part of Western Australia, I feel that some apology is due for laying

476 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

before them a work so imperfect in its composition and arrangement,
and I beg to state that I have only been induced to make the attempt
in consequence of the almost total absence of any published informa-
tion regarding the geological structure of this portion of the Austra-
lian continent *.

During a residence of thirty years in Western Australia, my ac-
quaintance with its geology has been almost entirely restricted to
the practical observation of its various stratified formations as pre-
sented to my view in the course of official and professional avoca-
tions, which led me over the whole of the known portion of this
province ; but, although thus enabled to accumulate a vast amount
of notes and details, I have not had the opportunity of classifying
them with any degree of certainty by the comparative study of its
geology with other countries where the nomenclature and limits of
the formations are well-known and established. The difficulty at-
tendant upon the collection and preservation of fossils while travel-
ling rapidly through a wild country has also been another obstacle in
the way of my endeavours to assign exact limits to the several for-
mations. It is therefore only since my arrival in England that,
through the assistance obligingly rendered me by Sir R. Murchison,
Dr. F. Hochstetter, and others, I have been enabled to deduce from
my paleontological observations any certain results, which, however,
although establishing a few main facts, it must be admitted leave much
yet to be done to render them complete, and which it is to be hoped
will shortly be followed up by more scientific observers; while the
present sketch is only to be viewed as a general outline to be wrought
upon by others following in the same path.

Having so far offered an explanation of the cireumstances under
which I venture to present to the Society the result of my labours, it
will now be my endeavour, as briefly as possible, to state a few facts
illustrative and explanatory of the topographical and geological fea-
tures of that portion of Australia illustrated by the map and sections.

Darling Range and the Country to the Eastward.—tThe principal
portion of Western Australia consists of an undulating table-land of
syenitic granite, and may justly be considered more continentalt than
eruptive. It has a western escarpment, which follows the meri-
dian line of the 116th degree of east longitude, commencing on the
south coast near Cape Beaufort, and already traced northward to
latitude 25° south on the Gascoyne River. The western edge of this

x A map and sections of a portion of Western Australia were presented to
the Geological Society by Messrs. J. W. and F. T. Gregory, Nov. 17, 1847 (Quart.
Journ. Geol. Soc. vol. iv. p. 142). The author also prepared a sketch-map of a
part of the geology of Western Australia (accompanied by sections), and placed
it in the hands of Mr. J. Arrowsmith, who, having engraved and published it at
his own cost, has kindly presented a copy to the Society, and liberally permitted
any use to be made of it. The sections at p. 477 are reduced from those engraved
with this map.

+ Though granite may not be anywhere eruptive, yet all granite was irruptive ;
but in Australia the old covering into which it was irrupted is almost completely
removed by denudation over very large areas. The term “continental” is pro-
bably intended to express this fact by the author, whose absence in Australia pre-
yents his revision of this paper whilst in the press —Enrr.

GREGORY— WESTERN AUSTRALIA. AT7

1861.]

Fig. 1.—Diagram-section across a part of Western Australia, in lat. 32° 8. Length about 40 miles.

=
8

West. Bd
=}

Perth

ES
Sp
fe Darling Range (1 00 ft.). 1500 ft.

p P P

a. Sand. f. Limestone with corals and shells; from | %. Yellow, blue, and white clays, containing
6. Ferruginous sandstone (Devonian ?). 200 to 300 feet thick. beds of limestone and ‘bog-iron-ore,
ce. Felspathic clay. g. Compact red sandstone. through which rise many chalybeate
d. White and pale yellow siliceous and cal- | ‘2. Variegated clay alternating with ferrugi- springs.

careous sand, occasionally containing nous sandstones. Cones and leaves of | 7. Blue and variegated yellow clay.

coral-limestone and beds of ferruginous Banksia occur rarely in the upper | m. Clay-slate.

conglomerate, from 100 to 150 feet in portion. n. Quartz.

thickness. z. Limestone. 0. Mica-schist.
é. Bog-iron-ore. j. Yellow clay. p. Syenitic granite, with numerous dykes of

serpentine, porphyry, and quartz.

Fig. 2.—Diagram-section across a part of Western Australia, in lat. 25° 15'S. Length about 200 miles.
ee, 4S gg m ys : Sea ee aca
23 zo FR ogg ee 22s fp Fs
ae Grey Plains. ag ry ker ce S835 oH qe
=e IAY VW QC TEX 7
k

a, Sand. ; sandstones, occur Ammonites, T; rigonte, | k, Granite, gneiss, and slate, with superficial

6 & c. Red drift-sand, 50 feet thick. and Pecten. deposits of granitic breccia, ferruginous

d. Sandstone. : J. Permian (?). clays, thin beds of saliferous sandstones,

e. Cretaceous (?). In this group, which g. Carboniferous (?). gypsum, calcareous tufa, and beds of

comprises both a white chalk-like (but | %. Devonian (?). nodular magnesian limestone. (Similar

non-calcareous) rock and ferruginous | 7. Metamorphic rock. deposits occur on the granite of fig. 1.)

VOL. XVII.—PART I,

478 PROCEEDINGS OF THE GEOLOGICAL society. = [ May 22,

elevation, for the first 300 miles on the south, rises abruptly from a
sea-flat or plain of small elevation, to the height of from 800 to
1200 feet above the sea, gradually ascending for 200 miles to the
eastward, to 1400 or 1600 feet, and in a few instances to 1800 and
2000 feet. Further towards the east it begins to dip under beds of
saliferous sandstone, ridges of fine red sand, salt-marshes contain-
ing beds of gypsum, calcareous tufa, and felspathic clays, which are
occasionally interrupted by small detached ranges of eruptive rock
capped with jasper, and beautifully striped red and black metamor-
phic sandstones. These ranges have a sharp rugged outline, rising
abruptly from the plains to an elevation of from 200 to 500 feet,
and seldom extending for more than two or three miles in length,
without any certain direction, although, perhaps, more frequently
running N.N.W. and 8.8.E.

The Western Coast.—Between the west escarpment of the table-
land or Darling Range and the sea, lies a low belt of country from
20 to 60 miles in width, the upper portion of which is evidently of
very recent formation, and at no very distant period has been sub-
merged under the ocean. From Flinder’s Bay northward to the
Moore River, this tract of country does not generally attain to a
greater elevation than from 40 to 200 feet, only reaching the latter
elevation when the action of the wind has driven the sands from the
sea into ridges running parallel to the coast. Those portions con-
taining a large amount of shelly and calcareous matter have since
formed, by the operation of water, into aggregations of more or less
compact limestone, which give a rugged outline to the hills near
the sea.

Proceeding northward from the Moore River, a nearly parallel and
lower branch of gneiss from the Darling Range diverges gradually to
the westward, appearing only in a few places on the Smith and
Irwin Rivers, forming a valley widening to the north, which contains
the coal-field of the Irwin; neither the valley nor the gneiss forms
a continuous line, being covered by an elevated tract of Cretaceous (?)
and Tertiary sandstone. The gneiss appears once more to the north-
ward in a detached mass, extending from Champion Bay to the
Murchison *River, forming the fertile and rich mineral district in
which so many valuable lodes of lead and copper have been discovered.
These lodes take an almost invariable direction of N. 32° E., with a
general dip of about 80° to the W.N.W., and are accompanied by
parallel dykes of whinstone, quartz, or porphyry, varying from a few
feet to 50 or 60 yards in breadth.

The gneiss here abounds in garnets, of rich colour, but much
flawed ; specimens of plumbago, tin-ore, antimony, and arsenic are
occasionally found. Specks of gold have also been obtained by wash-
ing the sands in the Bowes River.

Returning southward to Flinder’s Bay, the Sussex coast shows an
outlying range of gneiss rising towards the east from beneath the
superior deposits and extending from Cape Leeuwin to Cape Natural-
iste, thus forming a bold promontory which is joined to the main-
land by a low, ferruginous, sandstone formation of recent date. At

1861. } GREGORY—WESTERN AUSTRALIA. 479

Cape Leeuwin the gneiss is composed almost entirely of felspar,
forming a cliff upwards of 70 feet high, capped with water-worn
blocks, the remains of an ancient sea-beach. About fifteen miles south
of the cape it dips considerably, and the red sandstone shows itself
where the brooks have cut through the superincumbent coast-lime-
stone. Thirty miles from Cape Leeuwin it contains large quantities
of garnets; and their fragments, with titaniferous iron-sand, are
strewn on the beach for some miles.

At the Leeuwin, vertical veins of hornblende traverse the gneiss,
some of them 100 feet in width. The only other locality in which
the gneiss is developed to any extent is on the Pallinup River, east-
ward of King George’s Sound, and at Doubtful Island Bay, still
further east. No mineral lodes, however, have as yet been dis-
covered in these districts; but small masses of plumbago and garnets
are not unfrequent.

Igneous Recks.—The distribution of eruptive rocks is, as shown
on the map, very general. Of basalt the chief mass lies at Bunbury,
rising about 30 feet above the sea; it is rudely columnar, and con-
tains traces of copper in its natural joints, fractures, and cavities,
but net in its substance, leading to the belief that it cuts a copper-
lode below ; there is no rock seen in contact withit. A brown clay
adjoining contains water-worn quartz-pebbles, amongst which Ifound
an opalescent stone, the size of a large pea, marked within with
five spots in the form of a perfect cross [chiastolite?}. About five
miles south the basalt again makes its appearance, and at twenty miles
it crosses the bed of the Capel River, and finally crops out in a con-
tinuation of the same line on the south coast to the eastward of
Flinder’s Bay. At Mundejung, 11 miles south of Kelmscott (which
is a few miles S.S.E. of Perth), there is a small patch of basalt
protruding between the syenite and clay-slate. Detached fragments
are also found at King George’s Sound, and on the shores of Doubtful
Island Bay.

Quartz-veins.—Quartz-veins are by no means unfrequent at the
higher leyels, and take a general N.N.E. direction. The quartz is
mostly crystalline and lustrous; and, with the exception of the
veins accompanying the lodes of lead and copper, and at a few
places on the Upper Gascoyne, it is seldom cellular or of the peculiar
opake milk-white colour which characterizes the quartz of the gold-
fields of Victoria and New South Wales. The largest mass yet
found is on the face of the Darling Range, 5 miles north of Kelm—
scott, and forms a conspicuous mark as seen from the coast.

Slates.—The development of chlorite-schist and clay-slate is very
limited, and chiefly confined to the western escarpment of the granite.

Silurian Rocks ?—Of the existence of the Silurian system in this
province, I have hitherto been unable to procure any positive proots,
owing to the deficiency of fossils in the localities in which, judging
by analogy, there is reason to suppose it might occur. The Mount
Barren Ranges are the only position in which rocks are found bearing
any Silurian character, or holding that relative position with regard
to other formations.

Devonian Rocks ?—Following up the formations in what I have

2K 2

a2

480 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

assumed to be their regular order in the ascending series, as tabulated
on the map, we come to the compact felspathic clays, sandstone, and
ferruginous conglomerates that cap the greater portion of the table-
land of the Darling Range,—varying probably from 100 feet and
under in thickness (fig. 1). All my researches have hitherto failed in
detecting any fossils in this formation; but, from its resting imme-
diately upon, and blending with the upper surface of the granite,
and apparently resulting from the decomposition of the granite
itself, I am led to believe that it is much older than the stratified
sandstones further north, or those to the south and east of the
Stirling Range, and, except in a few places in its upper portions,
lower in the system than the Carboniferous formations on the Fitz-
gerald and Irwin Rivers.

Carboniferous Rocks——On the Carboniferous formation I would
only venture to offer the additional remark, in amplification of the
map and sections, that the coal on the Irwin River appears to be
almost immediately covered by the Cretaceous (?) sandstone, the Sali-
ferous or New Red being either very thin or altogether wanting (fig.3).
The coal-seams are well defined, and dip at a considerable angle ;
the specimens obtained from the exposed edges contain a large per-
centage of carbon, but are deficient in bitumen. On the Fitzgerald
River a true seam has not yet been found: the known bed is hori-
zontal, resting unconformably upon the edges of highly elevated
Carboniferous shales, and contains many distinct fragments of only
semifossilized wood and pieces of infusible resin; it is in imme—
diate contact with a band of green sand of several hundred feet in
thickness, similar in appearance to the Upper Greensand in the Isle
of Wight; but whether under- or over-lying, I could not ascertain
with certainty (fig. 4).

Cretaceous (?) Rocks.—The Cretaceous (?) are the most extensively
developed of the sedimentary rocks in Western Australia, and are
almost exclusively siliceous in character, containing only few beds
of chalk, of very inferior quality. They abound, however, more in
fossils than the Carboniferous do, and, with the exception of the recent
coast-limestone, more so than any other formation. Flints are rarely
found in them. The bed of the Greenough River is the best spot for
procuring specimens, although a few are found in the chalk-hills
near Gingin (spines of Echinoderms, &c.).

Anolian Rocks of the Coast—Turning to the coral-range that
borders a large portion of the sea-coast, especially on the western
shores, we have a remarkable instance of the constructive and accu-
mulative power of the wind. ‘The peculiar formation of these hills
renders it quite evident that they are more recent than the low plain
upon which they stand, as, when cut through by the rivers, they
present a bold wavy stratification, always more abrupt inland, the
prevailing winds being from the S.W. The bivalve shells imbedded
in them almost invariably lie with their concave faces downwards*.

* In these calcareous beds the following species are (on the author’s map)
stated to occur:—Dolium galea, Ranella granifera, Solarium perspectivum,
Seraphs terebellum, Conus marmoreus, Phasianella australis, Haliotis tuberculata,
and Bulla ampulla.

481

GREGORY—-WESTERN AUSTRALIA.

1861.]

Fig. 3.—Section of the Coal-seams on the Irwin River, Western Australia (lat. 29°8., ong. 115° 25’ E.).
Length about 220 yards.

About 400 feet above the sea.

j. Two coal-seams (5 feet).
g. Red sandstone. k. Black shale.

a. Coarse red sandstone (10 feet thick). Ff. Coal (2 feet).
6. Brown sandstone and shales.

ce. Red grit alternating with shales.
d. White shale.

e. Black shale.

h. White shale. Z, White shale.
z. Black and white shales and sandstone. m. Brown shales with black streaks.

Fig. 4.—Diagram-section of the Strata on the Fitzgerald River in the Southern portion of Western Australia
(lat. 34° 8., long. 119° 20’ E.). Length about 20 miles.

. About 3
- 800 ft. Mount Barren Ridge.
ow) Point © S.
eae Charles,
4

a. Granite. d. Coal, J. Metamorphic sandstones and jasper tra-
6. Sandstone. e. Contorted shales and sandstones (Car- versed with dykes of trap and quartz.
c. Sandstone with fossil wood and gypsum boniferous). g. Gneiss and granite.

(Cretaceous ?). )

482 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

Recent Elevation of the Land,—Of recent changes of elevation
there are but slight evidences. The numerous beds of oyster- and
cockle-shells, just above the present sea-level, of species still existent
in the adjacent seas, tend to prove that there has been a gradual
though slight upheaval of the coast since its first emergence from
the ocean. To this may be added the fact, that the remains of a
vessel of considerable tonnage have been discovered in a shallow
estuary near the Vasse Inlet, and now quite shut out from the sea,
which, from its appearance, I should judge to have been wreeked
more than two hundred years ago, during which period the land
appears to have risen about two or three feet. This, together with
the fact that within the known limits of Western Australia there is
not a single volcano, either active or extinct, nor any but slight
evidences of volcanic agencies having been at work, goes far to prove
that this portion of the Australian continent has undergone fewer
changes than almost any other part of the world.

Conclusion.—A careful digest of the preceding facts, together
with other observations, leads to the following conclusions, which
differ but slightly from some geological notes published in the
colony some ten years ago by my late brother, Mr. J. W. Gregory :—

First, that the Darling Range possesses no true anticlinal axis,
but is a sudden break and descent of the table-land of the interior
to the plain or sea-flat of Quartaina, which will account, perhaps,
for the non-appearance of the Silurian rocks, and for the very narrow
belt of chlorite- and clay-slates. Secondly, that the Darling Range
attained nearly its present elevation (that is, relatively to the other
strata, but not with regard to the sea-level) before the period of
the Coal-formation. Before the Carboniferous (or at least Upper
Paleozoic) period, the pre-existing rocks into which granite had
been largely irrupted were so extensively acted upon by denudation
as to be almost completely removed, their present surface-outline
being nearly the same as that which they had during the Upper
Palaeozoic period. On that surface the Carboniferous rocks were de-
posited unconformably. They were again denuded, and Cretaceous(?)
and Tertiary rocks were deposited unconformably on both. Since
then, the country has been both elevated and depressed, more than
once perhaps, but bodily and equably, and without tilting.

Note by the Eprror of the Q. J. G.S.

Besides numerous specimens of rocks and minerals, the follow-
ing fossils are comprised in Mr, Gregory’s collection brought from
Western Australia :—

Carboniferous fossils from Irwin River (with coal):—

Spirifer (two species). Nautilus.
Productus (two species). Cyathophyllum (small).
Pleurotomaria. | Encrinital stems.

Spirifer from Lyons River, East of Kennedy Range.
Coal (brown-coal) from Fitzgerald River, and a fragment of a Cyathophyllum
from “above the coal.”

1861.] MOORE—-RHZTIC BEDS AND FOSSILS. 483

Fossils of Secondary age ( Trigonie and Ammonites) from the Moresby Range ;
and an Ammonite in a soft, white rock (not calcareous) from the foot of
Mount Albert.

Pecten from Victoria Range, 4 miles Hast of Wizard Park, Moresby Range.

Fossil wood from the Moresby Range, the Stirling Range, and the Upper
Murchison River.

A small Ventriculite in flint from Gingin.

2. On the Zonus of the Lower Liss and the Avicula contorta Zone.
By Cuartes Moors, Esq., F.G.S.

[Puates XV. & XVI.}

ConrTENTS.
Introduction. Section at Steven’s Hill, near Long
§1. Lower Lias and Rhetic Beds of the Sutton.
neighbourhood of Ilminster. Section at Saltford.
Sections at Beer-Crowcombe. Other Sections in Somersetshire—
Sections at North Curry and Knap. Batheaston and Paulton.
§ 2. Subdivisions of the Lower Lias and Section at Westbury.
Rhetic Beds. The true position Sections in Gloucestershire and
of the “ White Lias.” Warwickshire.
Dr. Wright’s views of the position Sections at Lyme Regis.
of the White Lias. True position of the White Lias.
White Lias at Beer-Crowcombe. § 3. The Rhetic Formation,
Section at Street. § 4. The Rheetic Fossils.
Section at Stoke St. Mary. Description of the Fossils.

Section at Pibsbury. Appendix.

Introduction.—In a paper on the above subject by Dr. T. Wright,
F.G.S., which appeared in the ‘ Journal of the Geological Society ’ for
November last*, reference is made to the occurrence of the Avicula
contorta zone at Beer-Crowcombe, near Ilminster, and a list of the
organic remains from thence, amounting to thirteen species, furnished
by the Rey. P. B. Brodie, is given. In the year 1847 that gentle-
man accompanied me to the locality, when the fossils thus noticed
were obtained. Since that time I have much increased their num-
ber, and I have also been enabled to establish the exact relative
position of the Avicula contorta bed, which at the time of our visit
was not clearly known.

It was my intention to have noticed in detail the sections that I
give below in connexion witha paper which I am preparing on the
Frome district, and in which I should have shown that many of the
organic remains that are deposited in the fissures of the Carboniferous
Limestone, and associated with the Microlestes and other extinct
Mammalia, are derived from the Bone-bed and other beds of the
Avicula contorta group; but, as some time will elapse before that
paper is completed, and as the attention of both English and Con-
tinental geologists will have been directed to the above subject by
Dr. Wright’s paper, I have considered it important that any addi-
tional information in connexion with the interesting fauna and the

* Vol. xvi, p. 374, &e. + Loc. cit, p. 384.

484 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

exact positions of these beds should be at once communicated ; and
this is the more desirable, since, unfortunately for what otherwise
would have been an excellent and useful paper, that gentleman has,
in my opinion, either mistaken or reversed the proper order of the
lowest Liassic zones—an error attending it throughout, and which,
unless corrected, may lead to some confusion.

§ 1. The Lower Linas, §c. of Ilminster and the neighbouring district.
—Before noticing in detail the section at Beer-Crowcombe, a short
description of the geological features of the district may be useful.
These are to be observed in a walk from Ilminster through Beer-
Crowcombe to Curry-Rival, and thence passing to North Curry; and
thus within a distance of about ten miles the formations from the
Upper Lias to the Keuper sandstones may be studied.

At Ilminster the Upper Lias forms the summit of the hills, capping
the Marlstone or Middle Lias. The former beds are rarely more
than from 6 to 8 feet in thickness, whilst the stone of the latter, for
which the quarries are worked, has an average thickness of about
8 feet. Descending the hill west of Ilminster, towards the Bridge-
water and Chard canal, which leads to Beer-Crowcombe and Curry-
Rival, the escarpment of the Middle Lias is passed, the lower
members of this zone being rarely exposed. They consist of brown
and grey micaceous brick-clays, haying a thickness of about 130 feet.
On reaching the level of the canal, these have graduated into the
upper blue marls of the Lower Lias; but sections of these are also
rarely seen. In this neighbourhood they are usually covered by
thick beds of gravel, derived from the Chalk and Greensand of the
Blackdown range, a few miles to the south.

The canal for about four miles is continued on these Lower Lias
marls, which at Ashill, a little to the west, have been proved to a
depth of 80 feet. At Beer-Crowcombe the canal enters a tunnel,
excavated on the south side in the Lower Lias. It emerges again at
Wrantage, about two miles to the north, under a bold escarpment of
the variegated marls of the New Red Sandstone. As these forma-
tions have here been uplifted, with a slight dip to the south, a good
section of them was made in cutting the canal. It was from the
southern end that the few blocks of the Avicula contorta bed men-
tioned in the Rey. P. B. Brodie’s communication to Dr. Wright
were obtained. Its position will be recognized as the ‘ Flnty
Bed,” No. 81, of the accompanying section (p. 486).

Passing down the northern escarpment of the beds before-men-
tioned, and crossing the valley towards North Curry, the Keuper
sandstones, with their characteristic plant-beds, may be seen in the
roadside leading to Morden, dipping under the formations already
noticed; whilst a little north of the village another escarpment of
these Keuper beds stretches away, as far as the eye can reach, to-
wards Langport, bounding the alluvial plain which extends to the
Bristol Channel.

In one of the first blocks of Keuper I examined at North Curry I
was reminded of the Reptiliferous sandstones near Elgin*, by finding

* See Quart. Journ. Geol. Soc. vol. xvi. p. 446.

1861.] MOORE—RHZETIC BEDS AND FOSSILS. 485

in it an imperfect rib-bone. It also yielded traces of fish-scales
and plants. A character these sandstones possess in common with
some of the Scottish beds, particularly those of the Quarry Wood
range near Elgin, is that they contain a number of flattened pellets
of marl, which, on being weathered out of the stone by exposure,leave
on the surfaces of the blocks their rounded or oval casts.

At Knap, west of North Curry, there is a large sandstone quarry
in which the beds are lower than those just mentioned ; but the pas-
sage-beds between them are unknown. Sections are given below,
p- 486. At this place the beds are non-fossiliferous.

Sections at Beer-Crowcombe.—My friend Mr. Brodie, in his com-
munication to Dr. Wright on the beds exhibited at. the Beer-Crow-
combe quarries, remarks that “there are several thin beds of lime-
stone, but not so thick as those in Warwickshire*”’. From the
following section, which I made in the year 1850, it will be seen
that they are of much greater thickness and importance than his
remark implies, or than our hurried visit to them in 1847 enabled
him to realize ; indeed I know of no other section in this zone of
rocks fuller or more instructive.

Sections of the Beds in descending order.

At IumounstTer.

ft. in. ft. in.
DitjvGP 1LIPS soconocededeobaoncvasobe 8 0 sional impressions of organic
Middle Lias. “Marlstone ...... 8 0 PEMAINS aauecenuscrmesceneae 130 0
Various brown and grey mica- Lower Lias. Upper blue marls
ceous brick-clays, with inter- on the line of canal and at
calated sandstone and occa- Asha erences. FOCOHOE 80 0

At Brrr-CrowcompE—Mr. Hornibrook’s Quarry.

ft. in. ft. in.
Wegetanle soiliaes ane... 2 9 | 19. Glassy blue bed...............0 4%
i Bastard rock 2.22. .-cosssee+: OFA LOM Shale ssc thee aaa caer ont I &
Dupo tS) AYO SES 4 oa RRP Re Re eRe 1 8 | 21. Jack blue bed..............6- 0 10
3), IBevimnaal ioyel< con soconaccdonese Oe) IPRA ISI Oet Ke) a sopeeuopopdtioatéencoobe 0 2
SM Sale aH sca couewen ences 1 9 | 23. Mumbling bed............... 0 5
Dem AstancrOCkssescn eae: Osos 24es Shale ses here cusan ue. 0 2
Gm SHAE tak c av econensaccouseans 2 O | 25. Mumbling bed............... 0 6
(es Bastavdenockeencts sheen OMNI Shalens anteater esta siete 0 2
SPADA Ceo Mctaa seats scan etek ces 2 0 | 27. First Come-by-chance...... 0 3
oh IBGE LWT (LCESH sp consecseaosoc Oke ome h28kaShaler sain aecucnconcesenees 0 5
NOM Shale wavwenecbewnascbaten eats O 7 | 29. Second Come-by-chance... O 4
eB astardiocksscaseeae ens: ORP2 SON Shale teseesesneescaeeee Ceca 0 I
Le Salevia tht chetee aa ween 0 4 g (ol. First black rock..... 0 5
13. Second buff coat............ OPE ey S27 Shale vie ee enn taesc 0 1
We Shales: tonne once iene 0 2 | ‘88 | 83. Second black rock.. O 6
Gy WMawiiel lower COLNE acoonecocades 0 2 S :$ 4 34. Third black rock.... 0 6
UGa Shales cen eta eee OB S S| Bo anllensocconcusenensac 0 6
lee Bastardirocken meee 0 2 |% 8 | 86. Fourth black rock
GMS Hall says sc eecice eaenete 0 3} gy (bottom-bed)...... 8

* Loe. cit.

486 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

Continued in Mr. Vile’s Quarry.

ft. in. ft. in.
( 37. Hookstone clay. (Nu- 49* Shaleiseessetecsnseceeense ors
merous _ scattered 50. Paving-bed...........006 0 4
| Saurian remains.)... 2 0 Ol Shale. sR acess 1 4
38. Hookstone ..........6 0 8 O2sRed bed: scseseenseeses 0 4
Bh | oo sibalevenecessseccrese one OU 1G er ds Shale: tccsccceteceeecee 0 1
AMON Clayabaisie seine ae, O 43] 8 | 54. Black bed.........c000+ 0 4
z AT uSlialeteensecsteeoseseeees 0 10 = 55. Shale........ aposcooneoscc 0 6
6428 Thick burrs <...;scs.<ss O 9 | 8 ) 56. Clog-stone.............- 1 3
ip) Aden Shalense.:..cccese wiccane I O23) (Ole Shaletss..sscse-sreeeee 2 2
&# | 44. Milley burrs........... 0 53) & | 58. Red fire-stone.......... 0 5
Abw Shales.scscssecasetescoees 0 3 DOP Shalelscccst ceseceetetens ia)
46. Fire-stone..........0006 0 3 G0} Blue' bed: ....5. es. ew)
Ale Shalevesercesdeseeesceses Wy ge OU Shale secenceccssseceecae 2 0
48, Paving-bed ............ 0 4 { 62. Drm Stereccnensecsecegees 1 0
Continued im Mr. Banfield’s Quarry.
ft. in. ft. in
63, Shalew us cscs. sseuascevesas 110) , (72. Shale ....0-0.....ccceesee 0 2
g | 64. White GAs ests see asec 0 8] & | 73. White Lias...........,... 0 38
S | 65. Shale ...........-...0ee00 0°68), 74; Shales tet. ten aweeeee 0 3
w | 66. White Lias............... O° 6S } 75. White Tias..- fee 0 6
15 4 67. Shale ............-.000+0- O° Set ) 76: Shale: 20s 2ces.ccaeneee 0 4
Geen WRILOMINTAS ease nseerrens 0 3/8 | 77. White Lias............... Ie
= cc Shaleet acer wae 0 3|S | 78. Rubbly Bed ............ 0 5
E | 70. White Lias............... 0 2/© \79. White Lias (bottom-
\ 71. White Lias............... 0 6 bed). ae

The position of the “ Flinty bed” in the Avicula contorta zone
below was satisfactorily established by the united testimony of several
labourers who assisted in the excavation of the tunnel, by an ex-
amination of the waste-heaps, and by several sections in the neigh-
bouring escarpments.

ft. in. ft. in.
s 80. Grey shaly marl ... 5 6 84. Light blue marl...... 6 0
rS 81. “ Flinty bed” (very : passing into
Ss fossiliferous) ...... 1 O| & | 85. Variegated blue and
© 3 4 82. Blue shaly marl...... 3 0 = red Keuper marls,
= & | 83. Pale blue stone, with re with alabaster,
3 yegetable-likemark- | about 100 0
tome HEV) qacaonooaaaooode ie (

Sections at North Curry and Knap.—Following below the varie-
gated marls (the precise thickness of which is unascertained), come
in the Upper Keuper Sandstones of North Curry: thus—

Section in the Lane near the Church.

ft. in. ft. in.
Various beds of dull grey and Red marl) .3....c..c.caceceeeeseeesee 2 0
brown sandstone, enclosing Light blue marl _.......:.2--20.«« 0 3
nodules of marl, and contain- Compact red marl inthinlamine 5 O
ing Estheria, Plants, traces of Nodular marl ...........2..20000+ 0
Fish-scales, and a Reptilian ‘Blue marl !s. <2n.cc---e eee see eran 1730,
ONO ss cake caceaeheas ss case eee 3 6) Variegated red and bluemarl... 4 O
(The above thicken in their Red shale, with quartz-grains... 6 0

dip to the south.) Red and blue compact marls,
Blue nodular marl ............... DO), BOWE reas. are eunaree ae 40 0

1861.] MOORE—RHZETIC BEDS AND FOSSILS. 487

Section of still lower beds at Knap ; 13 male distant.

ft. in. ft. in.
Variegated marls ...............05 WMO SANGStONE) sewtanccwcaecocecense sees 1 10
DWeep=redamarlie. sc. jacnssseeree te 2 everclear lieceneancsnssseebcesmesese: 1 10
Chocolate-coloured marl ......... 2 4] Grey sandstone.............-...065- 2 2
Compact grey stone............... OD) AN DOS. CICRIMRBR RAE te Oean ok Aaaas A)
Greyemanl hee cseascercsecnarensee One) D onege Gori asc scccasscssseene 2 3
egal Tene Sa onqaetococeooodaupaanan Ge 1 2} Do. Lo arm ie eet 0 10
Garey rman) pens sceneasenncenere OO IDes Clo cosbopaccdanomchondan 3.6
Grey sandstone, thin courses... 3 0

The beds at Knap are covered by a drift composed of cherty
pebbles. They afford no indications of organic remains; but litho-
logically they present a close resemblance to the Upper Keuper
Sandstones of Worcestershire.

§ 2. Subdivisions of the Lower Lias, Fc. ; the true position of the
“‘ White Lias.”—In the division of the Liassic beds, Dr. Wright has
followed Dr. Oppel of Munich in adopting a series of Ammonite-
zones,—a plan which, though generally convenient, may not always
be safe, since it is probable that at any time the range of specific
forms may require to be extended.

The zones thus adopted (by Dr. Wright) in descending order are,—

2. A. oxynothus zone. Lias.

3. A. obtusus zone. Ostrea-beds.

4. A. Turneri zone. 7. Avicula contorta beds, Keuper.
5. A, Bucklandi zone.

1. Ammonites raricostatus zone. A. planorbis zone, including White
6

Between the zones 5 and 6 Dr. Oppel has placed a zone of the Am.
angulatus ; but this isa species that has a considerable range into the
other zones, and is therefore properly omitted. I do not take excep-
tion to any of the divisions above the Am. planorbis beds, but I pro-
pose inserting below those beds two other zones, viz. :—a Saurian zone,
and the White Lias zone of Mr. Smith. When I refer, therefore, in
the following remark to the “‘ White Lias,’’ it is to be understood as
everywhere occupying a position immediately above the Avicula con-
torta zone and at the base of the true Liassic series. Its position
seems to have been mistaken by Dr. Wright, who has, in my opinion,
been misled, by thequarrymen in the different localities,into supposing
that their local beds of “ White Lias,” or what would be a white-
looking band of stone in a blue-lias quarry, is the true White Lias of
Smith, which is a series of beds occupying a uniformly lower position.

I propose, therefore, the following arrangement :—

6. Ammonites planorbis zone.
7. Enaliosaurian zone.
8. White Lias.

9. Avicula contorta beds.

} Rheetic Formation.
10. Keuper marls.

In my section at Beer-Crowcombe, the beds Nos. 1 to 30, which
are superior to the Am, planorbis, represent one or more of the
higher zones; but, as at this place I have found no Ammonites in
them, their divisions are undeterminable.

488 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

In the remaining portion of my paper, the remarks I shall offer
will have more especial reference to the beds which Dr. Wright has
included in the Am. planorbis zone and to those following below. I
shall then show the desirability of adopting a different classification
for those he has included in the group characterized by the Avicula
contorta, which latter beds are placed by Dr. Wright with the Keuper ;
and finally offer reasons for removing them, with the “ White Lnas,”
to the “ Rhetic Formation” of Continental geologists.

Dr. Wright’s views of the position of the White Lias—When de-
scribing the zone of the Ammonites planorbis, Dr. Wright remarks
(loc. cit. p. 389) that “‘in general it consists of a series of thin,
greyish or bluish, argillaceous limestones, with alternating beds of
laminated shale; or sometimes the entire series forms a thick-
bedded, argillaceous, cream-coloured limestone, called the White
Inas, by William Smith. In the upper half of this group of beds,
Ammonites planorbis, Sow., is found in great numbers, compressed
in the shales, with its white shell more or less preserved ; in the
lower portion of the series, Ostrea liassica, Strickland, appears in
great numbers; and beneath these strata are three or four beds of
hard limestones (or ‘firestones’), in which the finest skeletons of
Enaliosauria have been discovered.”

Again, at p. 396 it is stated that the ‘“‘ White Lias series of the
section at Saltford (p. 400) represents the Am. planorbis beds: here
also the relation of that zone to the Saurian beds below, and to the
Am. Bucklandi beds above, is well shown.”

In the table given at p. 411 the following arrangement and de-
scription of the beds are adopted :—

( f. Greyish or light-coloured limestones, in thin beds,

x interstratified with finely laminated shales; the
: Zone of A. limestones forming the paving-beds of Warwick-
aay = planorbis. shire, and the White Lias of Dorsetshire, and con-
cea taining Am. planorbis, Am. Johnstoni, Lima pune-

a2 tata, &e.

a z | g. Hard dark-grey limestone, containing Ostrea liassica

Ostrea- in great abundance, with skeletons of Plestosawrus

& beds. l megacephalus, P. Hawkinsit, Ichthyosaurus tnter-
medius, and I. tenutrostris.

A h. Dark shales, with thin bands of limestones, often
£2, | Zone of pyritic, and thin beds of light-coloured micaceous
Sg aS Avicula sandstone, with a thin band of bone-breccia near
4 p= © | contorta. the base. These contain Avicula contorta, Pecten

\ Valoniensis, and Pullastra arenicola.

From the above extracts it will appear evident that Dr. Wright
has incorporated the White Lias of William Smith, Conybeare and
Phillips, and other geologists, with the Ammonites planorbis zone,

* Dr. Wright in this table has divided the Lower Lias into Ammonitiferous
and Non-ammonitiferous beds,—the former ending with his 4m. planorbis zone,
the latter including the Ostrea-zone (or true White Lias) and the Avicula con-
torta zone. ‘This division is not desirable; for, although Ammonites are rare in
the lower beds of the Lias, they are not altogether absent. I have obtained small
flattened specimens from the Saurian beds ; and Mr. Tomes informs me they are
also to be found through the whole of the Warwickshire Liassic series.

1861. ] MOORE—RHZETIC BEDS AND FOSSILS. 489

and has placed the Saurian beds either in or below the Ostrea-beds, the
latter being in fact the equivalents of the White Lias of those authors.

White Lias at Beer-Crowcombe.—On referring to the very full
section I have given of the Liassic beds at Beer-Crowcombe (p. 485)
the Am. planorbis zone will be seen to commence with the bed No. 31,
and appears to have a vertical range downwards to the ‘“‘ Hookstone
clay,”’ 37, lower than which I have not observed it. This Ammonite
is abundant ; and is sometimes found with the 7rigonellites in place.

Including the Hookstone clay just mentioned, in which there are
numerous scattered Saurian remains, all the beds following, to the
White Lias, may be said to constitute a Saurian zone, as these
remains may be found more or less abundantly throughout them ;
though, as stated by Dr. Wright in his remarks on the Street section,
to which I shall presently refer, the finest examples are usually from
the lowest beds.

Immediately below the Saurian zone will be found the true posi-
tion of the White Lias, whilst its continuation downwards into the
Avicula contorta beds is shown in my section; and beneath these,
again, are the variegated marls of the Keuper, and their underlying
sandstones.

Section at Street.—The most important sections from Somerset-
shire given by Dr. Wright are those of Saltford, near Bath, and
Street. The latter is distant about 14 miles in a direct line from
the one at Beer-Crowcombe. The names of the beds in the latter
locality are those by which they are known to the quarrymen. On
comparing the Beer-Crowcombe section with that at Street, although
the beds vary in thickness, which might be expected at such a
distance, a parallel may be observed between them, and some of them
are really called by the same names. Thus, in the Saurian zone of
the Street section, the Firestone bed, No. 29, and the Grey Clog,
No. 25, of Dr. Wright, occupy the same relative position, and are the
probable equivalents of the ‘‘ Red Firestone,” No. 58, and the “ Clog-
stone,” No. 56, of my section at Beer-Crowcombe. The “ Yellow
laminated clay,” No. 3, at Street answers the description and occupies
the position of the “ Hookstone Clay,” No. 37, at the latter place ;
whilst, reckoning from the base of the Saurian zone to the highest
bed in the Am. planorbis series, there is a difference of only one in
the number of beds in the two sections. The quarries at these
localities are therefore undoubtedly on the same horizon. They are
chiefly worked at both places for the paving-beds, the best of which
are found in the lowest part of the Saurian zone. I have no doubt
that, had the section given by Dr. Wright at Street been continued
downwards, the White Lias, as shown in my section at Beer-Crow-
combe, would have been found.

Section at Stoke St. Mary.—In order still more clearly to point
out the invariable position of the White Lias, I give particulars of a
section occurring at Stoke St. Mary, near Taunton, which I have
lately had an opportunity of visiting in company with the Rey. W.
A. Jones, F.G.S. This section is some miles south-west of that at
Beer-Crowcombe. Although slight discrepancies will appear, nearly

490 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

all the lower beds are called by the same names, occur in the same
order, and are usually of the same thicknesses as those at Beer, and
Saurian remains are found in the same zone as at that place and at
Street. :
This section is the more interesting as the workings are carried
down through the Saurian zone to the lower beds of the White Laas.
For the sake of comparison I have appended to the Stoke St. Mary
beds the numbers they represent in the Saurian zone at Beer-Crow-
combe. The White Lias beds vary much in different localities.

Section at Stoke St. Mary.

ft. in. ft. in.

Gravellcnec osnter: 5 0 DOs Shales. si. -ancsscaeceas 0 9

Bee) (jecenateyy Milas pana. ODO so (GO>Bluesiiasie- essere Leet
ess OD. Shale Uses. cadnesse- 1. (Ose) 5| GL. Shalewsine aay eeeeees 3.0
SN | 36. Pap-meat ......... O68 Ne NG25 Dunsterte espera 10
ime Sues bale) eee eekenee ane: V2 S61632) Shale cassosessenceeneeeee 1 8
38. Rough Blue bed... 0 10)"§ | 64. Blue Lias ............... OF9

39. Blue shale ......... 1 6) & | 65. Shale.....-........-2..-+- 0 2

40. Clay-bats............ 0 6 66. Blue Lias ............... OF

SLivaille) Waseansdnoscone 0 6 \.675) Shale Jocs<aensaeceacesee 0 3

[Several beds not Buckles-o. ss seuc-cs-cseeeeeeee 0 2
recognized here. | Top-size White Rock...... 0 6

44. Sandstone ......... 0 4 Shale). jaccteeanceee exten 0 4
esleosis balled yeediecneenseae 0 2 Second-size White Rock... 0 6

& | 46. Sandstone ......... 0 3) 5 | Shale .......... Jonsson eens 0 3
NE PATGr ales lstscas ae snes 1 6) 8 | Third-size White Rock... 1 0
& < 48. Paving-bed......... QO) EINE shale a. i... oeaecaeaneene 0 1%
| 49. Shalpweicaiin a... O 3) $ | Thin stripe so... cece 0 14

& | 50. Paving-bed......... OF Ay) Shaler o.c cc.) aachneaosoacaee O21!
Bl elavchaleie cee ruses: 1. j3).2 | hin stripe cnscst eee 0
52. Sandstone ......... 0 4 = Fourth-size White Rock 1 1

Day OUI Ue enasteesecee 0 2 SL MAE soanseddoanbadcasnopncer 0 2

54. Cockle-bed ......... 0 8 GrabiRock “reaccmse-eees 0 9

DOM SBalolersecee.veter= 0 2 Shalen i: .-.ceperoseseosaestaeee 0 3

56. Clog-stone ......... 0 8 Dunster Bags .........06005 0 3

57. Firestone-clay ... 2 0O Dunster Bags ........--..00 One

58. Firestone ......... 0 4

No direct passage leading into the above-mentioned beds from the
red marls is to be observed in the escarpments, and therefore no
trace of the Avicula contorta zone. Wells have been sunk to a depth
of 60 feet in the marls, to obtain water. In the sides of the turnpike-
road leading to Taunton, thin beds of Keuper are present with Posi-
donomya minuta,

Section at Pibsbury.—In addition to the sections already enume-
rated, there are numerous quarries in which the lower zones of the
Lias are worked in the district south of Street, at King-Weston,
Keinton, Sparkford, Somerton, and on the line of road between
Langport and Long Sutton. Langport is on the Keuper; and on
ascending the hill from thence to Huish-Episcopi, the White Lias
beds are exposed in a roadside-cutting, and in an adjoining quarry.
These beds dip to the east, and at a mile and half from Langport,
pass under others which are worked on the same line of road at
Pibsbury, a section of which, given below, shows that the latter are

1861. ] MOORE—RHETIC BEDS AND FOSSILS. 491

undoubtedly on the same horizon as the beds given by Dr. Wright
in the Street section, which are distant about ten miles.

Section at Pibsbury.

Equivalent Equivalent
bed at bed at
Street. No. ft.in.| Street. No. ft. in.
le 1. Corn-size ......... 0 6 18. 14. Shale ............ 0 2
8. De Shale sues csceocs 0 3 19. 15. Black bed......... 0 7
9. Sehinebedessssees: 0 4 20. 16. Shale ............ 0 7
10. Av Shale vases antes a 0 4 21. 17. Pig’s Paviour... 0 3
ie 5. Milley-burrs 0 6 225) Ss Shales eeeeeesea:. 0 3
12. Gashalew eect: 0 6 23. Los blueiClops ies. 10 Ut
7. Bunch-back...... 0 4 24. 2°20) Shale ey ee! 2,
Su Shalercs-teescess 1 0 25. 21. Dun Paviour ... 05
13 9. White stone ... O 4 (Grey Clog) a
~ | 10. White stone O 4 27. 22. Pond-size......... 5
eel Shales screens 0 10 28. 23. Lias-paviour ... O 4
15. 12. Cream-bed ..... 0 2 29. 24. Tomb-size ...... 0 6
16,17. 13. Firestone........ 8) 30. 25. Bottom-bed ...... O 4

In this section the beds 1 to 6 of Street, which would represent
the Ammonites planorbis zone, are not present.

A quarryman at Pibsbury had also worked at Street, and was able
to correlate the beds with those in that locality, and to point out
their local variations. Thus, he informed me that the “ Bunch-back ”
and underlying shale (Nos. 7 & 8) were wanting at Street; the
«White stone,” instead of being one bed, was divided into two, and
that the “ Firestone,’ No. 13, was the “ Red Liver” and “ Black
bed” of Street (Nos. 16 & 17) “run together.” Inquiries of the
quarrymen working in this zone of rocks, for the White Lias, gene-
rally resulted in the remark that they did not work down to it.

Section at Long Sutton.—Passing to Long Sutton, about two miles
further on, the same beds are again worked, in a quarry belonging
to the Earl of Burlington. A fault at the west of this village has
brought up the White Lias beds, the position and thicknesses of
which are admirably shown in a section worked almost entirely in
this zone at Steven’s Hill, in which between the Saurian zone in the
quarries just mentioned, and that of the Avicula contorta, not less
than thirty-five beds of White Lias are exposed.

Section of White Laas at Steven’s Hill, Long Sutton.

ft. in. ft. in.

1. Splintery beds of Blue Lias UN (Shall epson fasaechensare cies 0 4
(bottom of the Saurian 12. White Lias .................. 1 0
ZONE)! vaciecoeecnsceetioses QisO hls Shale: kts .chvwessece seen 0 2}

Peet S 0A Grae senna Sa eA REA ZO ASI NViniteg lias) eiceeesacusaceee 0 5
an Wilnite Taal: sani fas soe sone OM Sie eLoy Shale cea cies mae ses 0 2
Shalev. Wcoaioac sud cdanyoencs SHOP | P1Gse Wihitevialas i. .vecsssnceesee O 23
DasWihiteWias paeceeaacsee eae OP Se WEG ASWale ox aeacecnsmtencecadce 0 43
G: Shale: [deca ieseseee eset ON Gy | TS Wihite Mash ve ccsas.raceess: 0 3
(eawiitesniasivesrae-ceesercs AROSVGI LOW Shales tse ak ee aeteene 0 6
Swshale fascias seme ee e278 2OS WV nite Pitaal eet ce oateem arco O 74
Sh NWO BEES scascocosuosoacess ONO) 21e* Shalorniveacecsteescens ORT
10. White Lias ..... L isgaeaaegan O 5}|22. White Lias .................. 0 23

492 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

Section of Whate Lias at Steven’s Mill, Long Sutton (continued).

. in.
Z3 Shales iacy.cnaee causes On VSL a Shale Goce se sassee nero neeee O Of
DA SAWihiteilasiennceruceteenc nee QO 24) 32. White Lias . ............0005 0 2

2on Shale wie eaereencae as O 3 | 383. White Lias ...............00 0 9

QGAiWihiteWiiasmseeseseceee tees OG.) 84s Shale’ ee eee 0 3

PA favo oe eM isedonguccdoadaddseracedt 0 7 | 35. White Lias .................. 0 8

Pésh \yifanirs) I DIEYS Gonoosdossnedspose 0 6 | 36. White Lias—Bottom-bed 1 3

29. White Lias (Coral-bed) ... 1 O | 37. Blue Marl ................. 5 0

SOM White siuiasmresasrneceec creer 0 6

Since my paper has been prepared, Mr. Kershaw (a section of
whose quarry at Wilmcote is given by Dr. Wright) has been through
the district accompanied by Mr. Tomes of Welford Hill, both of
whom are well acquainted with the Warwickshire beds. After their
examination, they entirely agree with me that the true White Lias
occupies a lower position, and is quite distinct from the Street beds.
They were fortunate enough to make out a fact that had escaped me
in the Steven’s Hill section,—namely,that the bed No. 29 contamed
a great number of Corals, most of which, having become decom-
posed, have left nothing but their casts in the stone, though in a few
instances the Coral is preserved.

In a note to me, Mr. Tomes describes it as a “‘ branching species,
several inches in height, with an epitheca having numerous and
regular concentric wrinkles, and delicate but distant longitudinal
strie ; probably of the genus Cladophylha.”

Section at Saltford.—In the section at Saltford (1. c. p. 400) con-
structed by Mr. W. Sanders of Clifton, the position of the White
Lias series is correctly given, though I should be disposed to include
in it only the beds Nos. 9 to 22. In a reference to his section (l. ¢,
p- 396), the Saurian beds are supposed to follow beneath the White
Lias; but in this section, as at Street and Beer, they are represented
by the limestones and shales above.

If there be any zone more persistent than another, it is that of the
White Lias. Wherever the Avicula contorta beds are exposed, the
representatives of the former may be expected to be present imme-
diately overlying them.

Other sections in Somersetshire.—In addition to the sections already
mentioned, others in which these beds may be found occur at
Fivehead, Hatch, Uphill, Somerton, and in a deep sinking for coal
at Batheaston, made in 1812, through the whole Liassic series, a
section of which is given at p. 262 of Conybeare and Phillips’s
‘Outlines of Geology of England and Wales.’ Near Bristol they
occur at Cotham, Bedminster, and Pylle Hill. In a paper* on the
Linksfield shales, I pointed out the correlation of those beds with the
latter section, and the presence of the White Lias zone occupying
the same position, as far north as Elgin.

Sections at Batheaston and Paulton.—In the section given of the
beds at Batheaston, p. 262, of Conybeare and Phillips’s ‘ Outlines,’
under the head of the “ Upper Marls” are included all the beds of

* Quart. Journ. Geol. Soc. vol. xvi. p. 445.

1861.] MOORE—RU TIC BEDS AND FOSSILS. - 493

the Upper Lias, the Middle Lias, or Marlstone, and also the Upper
Marls of the Lower Lias, with some of their limestones, having
altogether an aggregate thickness of 220 feet. Then follow what
those authors (C. & P.) call the “True Lias beds,” including the
White Lias at its base; and their “ Lower Marls,” down to the New
Red ground, include the Avicula contorta series.

Section at Batheaston.

ft. in. ft. in
( Upper Marls ............ 220 O Blue Marl ............++- 6
3 Hard rock ..........0060 18 4 Stonern eee rates 0 6
Pee BIG) BONO)... .15..c0sc's+ BL] gg | Clay ceveeeseseeceeeteeees 0 9
38 | Hard blue stone......... UB aL Ses Rough blue marl ...... 0 5
ra Stoner nic sccrust-ncssne 2 0/8 Ss Black marl . ..........+0« 10 0
White Lias rock ...... 10 0 Light-blue marl......... 20
Red ground of New Red

Sandstone (Keuper).

A section also of the beds at Paulton near Bath is given on the
same page.

ft. in ft. in

Inferior Oolite ...... 18 0 Blue marl ............cceee eens 6 0

Upper Lias marls ... 120 0 Claystone, &C. ......seeee eee 3 0

ow g | Grey and blue Lias Black imarlterceciescssecesster 6 0
E29 VOCS sc aisivaess aeerne 6 0
Evetom| Sun bed! s)...f...1.0.., 1 6
Vag? JUHES eooodeccede: 12 0

Section at Westbury.—Dr. Wright has given a section of the
Avicula contorta zone at Westbury, which commences in the Ostrea-
bed, described by him as being one of the lowest in the “Am.
planorbis series,” but which, I consider, belongs to the true White
Lias, and is equivalent to those beds at Saltford, Beer-Crowcombe,
Stoke St. Mary, cc. :

In this view I am again confirmed by the above-mentioned
authors, who at p. 263 of the ‘ Outlines,’ &c., give the following
section at Westbury-on-Severn.

Section at Westbury-on-Severn.

ft. in
ULES OLES + aca peconB eR OBC ROMEO BET Hac iOGH OOH SOB CEBENO Rec E ape OCI auuCOE 10
2 ASIC ISHALE We Sutin ata estes eect ASA aeRO Ace meek anon cauee ne estan tel 10 0
3 TSIRVO. Bar femecer crn Bae cane ete Gane EE ane ae corr A Lae assert 12 0
$ «| Gueen siliceous grit, containing abundant bones, well known,
3k here and at Aust, as the bone-Bed............s.sssseeeeeeneesenneetes ew)
Seen nace shit omenaars cnet ee coahk soracerassctoesasscoessciesbceieur soeevsenaves 2 0
3 Grcemyrri lpn ttie ner as mime ween Meee anita ny eu MAU ae ad eww cdae tes 0 6
si Blacks shiale wey, ee unsae mal: AU a wee NaN Rr ESR ie 2 0
Greenish marlstone and red marls of the Keuper ..........s-..00+8 18 0

In all these sections it is thus seen that these authors place the
White Lias as a distinct zone immediately overlying the A. contorta

* Over this portion of the Somersetshire coal-field many of the beds are
much reduced in thickness. The Middle Lias, for instance, which in some parts
has a thickness of upwards of 100 ft., is here represented by beds of but 4 or
5 feet in thickness; and the upper beds of the Lower Lias are also wanting.

VOL. XVII, —PARI I, 21

494. PROCEEDINGS OF THE GEOLOGICAL SOCINTY. [May 22,

bed, in which the beds correspond with every other section with
which I am acquainted. 4

When speaking of the White Lias, they say that it takes a high
polish, and may readily be employed for lithographic purposes, a
description which corresponds with that given of the beds at Lyme
by Dr. Wright.

Sections in Gloucestershire and Warwickshire.—I am unacquainted
with some of the sections in Gloucestershire and Warwickshire given
by Dr. Wright; but in that at Aust Cliff, I am disposed te consider
the nine beds above the Avicula contorta zone to be the representa~—
tives of the White Lias, and not of the Am. planorbis zone. In
Warwickshire, the best section is afforded by the quarry of Messrs.
Greaves and Kershaw, at Wilmcote, near Stratford-on-Avon (op.
cit. p. 886), in which the beds are shown to be very similar to those
at Street. My correlation of the latter beds with those at Beer-
Crowcombe being admitted, it will at once be evident that in this
locality the upper beds, Nos. 1 to 7, represent the Am. planorbis
zone, and Nos. 8 to 28 or 24 the Saurian zone, whilst the “‘ Hard
crystalline limestones,” d&c., which follow, are in all probability the
representatives of the White Lias. With this arrangement the cor-
relation of the zones with those at Street and Beer-Crowcombe is
established.

On referring to a note which I some time ago received from Mr.
Tomes, I find that he recognizes the position of the White Lias of
that district when he says: ‘‘ The Warwickshire White Lias appears
to represent a different zone from the Somersetshire White Lias,
being very low in the series.” He then points out its position by a
rough section, in which I recognize it as occupying the same zone as
in all other localities. The position of the Avicula contorta beds is
in every case correctly given by Dr. Wright, as following at the base
of each section, lying above the Red Marls.

In the neighbourhood of Tewkesbury, Dr. Wright states there are
several good exposures of the infra-ammonitic beds (meaning those
below the Am. planorbis zone), from which were obtained numerous
fine examples of Jchthyosauri and Plesiosauri, and that he possesses
vertebrae of Plesiosaurus rugosus from a bed of White Lias at Wool-
ridge Common. These beds, again, are evidently on the horizon of
the Saurian beds of Somersetshire ; and although the bed at Wool-
ridge Common from whence the Plesiosawrus was obtained may be
a white-looking lias, it is not the basement White Lias zone, in
which, as I have elsewhere stated, no Saurian remains have eyer
been found.

Sections at Lyme Regis—The chief point of interest advanced by
Dr. Wright respecting the Lyme section is that in which he places
the Saurian zone, not on the horizon of those beds in Somersetshire
and Warwickshire, but in the Am. Bucklandi zone which overlies
them. Itis notimpossible that circumstances may have been favour-
able to a larger development of Enaliosaurian life in the Liassie
seas at the point where these beds are now found, especially when
it is considered that their remains are occasionally, though but

1861.] MOORE—-RHZTIC BEDS AND FOSSILS. 495

rarely, found in the same zone elsewhere; but, supposing those
given by Dr. Wright in his section (p. 401) at Broad Ledge to be the
true equivalents of his Ammonites Bucklandi beds at Street (p. 390),
there would still have to be accounted for at Lyme the Am. planorbis
zone, and my “ Saurian beds” below, which, in such a development
of the Lias as occurs at Lyme, can scarcely fail to have their repre-
sentatives.

Two sections of what Dr. Wright considers the Am. planorbis
zone are indeed given, one of which is at Up-Lyme, the other at
Pinhay Bay. In their description, the stone is stated to be ‘‘ cream-
coloured, and so hard and close-grained that it might be used for
lithographic purposes.’ This answers precisely to the character of the
true White Lias ; and I have little doubt that it is such. Its place is
therefore on the zone of that series as given in my:Beer-Crowcombe
and Stoke sections, and in that (described by Dr. Wright) at Salt-
ford, where it immediately overlies the Avicula contorta beds. It is
therefore much lower than the Am. planorbis beds. It then appears
to me that neither the latter zone nor the Somersetshire Saurian zone
has been recognized at Lyme by Dr. Wright; and in this case, I
should incline to the view (should the whole of the Lyme section
have been given) that some of the lower beds which he has classed
under the Am. Bucklandi zone may be their representatives, even
though it necessitated giving to the Am. Bucklandi and other shells
a greater vertical range than they have hitherto been supposed to
attain.

Prue position of the White Lias.—I have thus shown that the
White Lias occupies a position at the base of the Liassie formation,—
that, of all Dr. Wright’s sections, its true place is only recognized at
Saltford, though here—and also when he notices the same zones at
Lyme, Wilmcote, &c. he confounds them with the Am. planorbis beds,
—and that intermediate between the White Lias and the latter are the
Saurian-bearing beds. To illustrate the difficulties created by these
transpositions, I need only remark that, whilst in the sections gene-
rally Dr. Wright places the Saurians in the Am. planorbis zone, at
Wilmeote he places them in the Ostrea-beds, or true White Lias, at
the base of the formation; and at Saltford he places them below
the White Lias, where only the Avicula contorta beds are to be
found,

$3. The Rhetic Formation—In the preceding observations I
have throughout referred to the White Lias zone as constituting a
member of the Liassic formation, with which hitherto it has always
been associated. I now propose its removal from that formation,
and its classification with the Avicula contorta group, under the above
designation. For this proposal my reasons are, Ist, that over a very
extended area the “‘ White Lias” forms a very persistent line of
demarcation, and is almost invariably present, overlying the Avicula
contorta beds wherever they are exposed; 2nd, that by its colour
and lithological character, being dense and close-grained, it forms a
marked contrast to the large flagey Saurian limestones of the Lower
_ lias immediately above; and 3rd, the great distinction which is
212

496 PROCEEDINGS OF THE GEOLOGICAL society. § [May 22,

presented by a consideration of the faunz of the two zones. In the
** White Lias”’ the organic remains are rare, and of very few specific
forms. Ostrea liassica, Strickl., Plicatula interstriata, Kw., and
Modiola minima prevail, and also characterize the beds below ; whilst
from other districts may occasionally be added Monotis, Lima, Cypris,
Estheria, and a few small univalves (usually in casts) of doubtful
specific forms, but which appear to have their representatives rather
in the Avicula contorta zone below, than in the “paving-beds ”
above; and it should be remembered that when these latter beds
were being deposited, the ocean teemed with Enaliosaurian life, of
whose presence in the “ White Lias”’ I as yet know of no evidence.

The “* White Lias”” presents evidences of a slow deposition; and
each bed appears subsequently to have been subjected to erosion.
The surfaces of many of the blocks are covered with Cypride. A
period of rest between the deposition of the several beds is shown
by the presence of colonies of boring Mollusks, which have left in-
numerable tubular perforations passing downwards in the beds.

Following the above, there would then be included in the “ Rheetic
formation ” all the beds lying superior to the variegated marls of the
Keuper,—the most noteworthy being the shelly bands yielding the
Avicula contorta, and the Bone-bed. Until lately these were included
with the Lower Lias; but, the investigations of Sir P. Egerton,
Agassiz, and others having demonstrated that the latter bed con-
tained a peculiar fauna, they have become recognized as 'l'riassic, or
as upper members of the New Red Sandstone, and they are retained
in Dr. Wright’s Table of Strata (op. cit. p. 376) as the uppermost
zone of the Keuper.

Meanwhile there have been discovered, on the continent, beds of
great thickness between the Lias and the Keuper, the representatives
of all of which were apparently wanting in this country.

In ascending order these are:

Ist. The St. Cassian and Hallstadt beds (which have yielded more
than 800 species of Mollusca); and

2nd. The Késsen stage, or, as it is now proposed to be termed by
Mr. Giimbel the State-Geologist of Bavaria, the Lthetic formation,—a
designation recoenized by Professor K. Suess, of the Imperial Museum
of Vienna, and which it will be convenient to adopt for the beds
under notice, which nm. this country are the representatives of the
second stage. In this division are comprehended the ‘ Deposito
d’Azzarolo’ of Italian geologists, as well as the Starkenberg beds
and Dachsteinkalk of Austrian geologists. In the Austrian Alps the
formations above noticed attain a thickness of from 4000 to 5000
feet. This is the important series of rocks of which, in this country,
the beds before referred to (rarely averaging more than 35 feet in
thickness, and intervening between the Lias and the Keuper) are the
diminutive representatives.

$4. Rheetie Organic Remains.—The organic remains in this forma-
tion in England are derived chiefly from the Bone-bed and the beds
yielding the Avicula contorta. At Beer-Croweombe the Bone-bed
appears to be wanting; but a few fish-remains that usually accom-

a

1861.) MOORE—RHZETIC BEDS AND FOSSILS. 497

pany it will be noticed from the latter bed at Beer-Crowcrombe. I
have assembled a remarkable fauna from a drift (derived from the
Bone-bed) near Frome, an account of which I must reserve for another
occasion. As, however, I shall have to notice below some Mollusca
from the Avicula contorta zone of this neighbourhood, I give a short
description of a very remarkable section in which those beds occur.

In the Vallis, near Frome, there are quarries worked for the Car-
boniferous Limestone, some of the beds of which have their up-
turned edges capped with horizontal Inferior Oolite. In a section
near Hapsford Mills I noticed a conglomerate with a few thin inter-
mediate layers of stone and clay. The limestone in this section has
a dip of 35°, N.W., and is worked toa depth of 15 feet. Lying upon
it there is a band of blue clay 4 inches in thickness, which, on close
examination, I found to contain a very interesting fauna. Associated
with remains of Fishes and Reptiles of the Bone-bed age, it yielded
Avicula contorta, Ostrea interstriata abundantly, Pecten Valoniensis,
with other genera never before noticed in beds of this age, such as
Chiton, Pollicipes, &e. This clay is succeeded by a dense conglome-
rate of rounded siliceous pebbles, 2 feet thick, and containing, though
rarely, fish-teeth and scales; another blue clay of 4 inches succeeds,
but without organic remains; then a grey conglomerate, 4 inches,
upon which there are courses of grey or cream-coloured nodular
limestone, intermingled with a grey clay, 1 foot in thickness. In
this, organic remains are extremely rare. Specimens of Lstheria,
Insects, and one block containing Plant-remains are all I have ob-
tained. Above the latter are beds of Inferior Oolite, 12 feet in thick-
ness, conglomeratic at their base.

The interposed beds of conglomerate, stone, and clay between the
Inferior Oolite and the Carboniferous Limestone, although but 4 feet
in thickness, may represent in this section the geological eras of the
White Inas, the Estheria-beds of Warwickshire and Gloucestershire,
the Avicula contorta zone, and the Bone-bed; so that, were the
“White Lias” to be considered to represent a distinct formation,
not less than four geological eras would be exhibited in one section
of about 30 feet in depth.

A thin band of conglomerate, 14 inch thick, of precisely the same
aspect, and the same age, is present in the Uphill railway-cutting.

Dr. Wright remarks (op. cit. p. 409) that he has “ shown that the
Conchifera axe special” to the Avicula contorta zone. In the blue
clay lying between the conglomerate and the Carboniferous Limestone
the Ostrea interstriata is the most abundant shell. It is found with
the Avicula contorta, and the Fish- and Reptile-remains before
alluded to, which represent the Bone-bed stage. The Ostrea inter-
striata is one of the characteristic shells of the ‘‘ White Lias”’ zone,
and furnishes an additional reason for including it with the Rhetic
beds.

The Avicula contorta zone, from whence the other organic remains
were obtained, will be recognized in the Beer-Crowcombe section as
the “ Flinty bed,” No. 81. It is composed of a dense, light-blue
stone, 1 foot in thickness, with alternating shelly layers,—the shells

498 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

being in most beautiful condition ; and in this they differ from those
found in almost every other locality in this country, as also from
those on the Continent. Dr. Wright has given a list of species (at
p. 385) from Beer-Crowcombe. He supposes (p. 377) that the shells
of this zone represent both the Késsen (or Rhetic) and also the
Upper St. Cassian beds. For some time I held this view; but, on
comparing the series I had made with that from the latter formation
in the British Museum, I was surprised by not finding a single
species in common; and I have since learnt that these stages have
a fauna quite distinct, and that the species found in the Avicula con-
torta zone and the Bone-bed in this country are identical only with
those of the Rheetic beds of the Continent, none of them being found
in the St. Cassian beds below.

Norves on THE Fossits.

It has been previously remarked that I have not observed the
Bone-bed at Beer-Crowcombe; but a few fish-remains are found in
the Avicula contorta zone, which are common to the Bone-bed when
it is found in other localities. In the thin band of blue marl in the
section at Vallis, fish- and reptile-remains are more abundant than
at Beer-Crowcombe ; but a detailed notice of these will be reserved
for a general paper on that district. I shall then be able to show
that the genera and species from the Avicula contorta zone at Beer-
Crowcombe are common to the same zone at Vallis, and also to the
Rheetic Mammalian Drift near Frome. It is important to recognize
their presence in this zone at Beer-Crowcombe, as they will assist
to determine the ages of the beds from whence that drift has been
derived, and therefore the probable age of the oldest known Mam-
malia of England.

Sarcopon romicus. Pl. XY. fig. 1.
Sargodon tomicus, Quenstedt ; Der Jura, tab. 2. figs. 34, 35.

A tooth, with a black, enamelled, semitransparent, canine-looking
crown, the inner side of which is concave, the outer slightly convex
and surmounted by a straight, sharp cutting-edge, in the largest
specimens two lines across. In the worn specimens the centre of
the crown is hollowed, usually with a slight sinus, dividing it into
two equal parts. A very young, unworn tooth from Frome shows
the crown in that stage to have been surmounted by three raised
cusps of equal size. Below the crown, which occupies about a sixth
of the height of the tooth, there is a long, slender, cylindrical, hollow
shaft, showing in some specimens a slight tendency at the base to a
fang-like division. They vary from 8 lines to 2 lines in length;
breadth 4a line to 2 lines. One example only has been found in
the “ Flinty bed” of Beer-Crowcombe ; from the Mammal-drift
near Frome I have many examples. It is interesting to find that
similar teeth were found by Pleininger with the MJccrolestes antiquus
at Wirtemberg, and that they should in this country be found in

1861. ] MOORE—RHZETIC BEDS AND FOSSILS. 499

the same association. The generic designation of the teeth above
noticed is from the existing genus Sargus, which possesses somewhat
imilar incisor-like teeth*.

Seuvatorata, Riley & Stutchbury.

Four fish-vertebree belonging to this genus have been found in the
“ Flinty bed” at Beer-Crowcombe. ‘These also occur in the Frome
Mammal-drift, where they are abundant.

There are also teeth of Lepidotus, Saurichthys acuminatus, S. api-
calis, Acrodus minimus, and scales of Gyrolepis, all of which are
found at Frome, and also a few undetermined fragmentary bones.

Mollusca.

Discrva TownsHeEnnr, Davidson.

In a paper on some new secondary Brachiopoda, in the ‘ Geologist ’
for March last, I mentioned the occurrence of this rare species in
the “ Flinty bed ” at Beer-Crowcombe, from whence I have but one
example. It is the only Brachiopod that has yet been noticed from
beds of the Rheetic formation, in situ,in this country, though I have
Lingula, Spirifer, Terebratula, and Rhynchonella from the Frome
drift. Terebratula, Rhynchonella, &e. are not uncommon in the
Rheetic beds on the Continent ; and Professor Suess informs me he
has found the Discina Townshendi in Austria.

AvictxLa contort, Portlock. Pl. XV. fig. 10.

_ The abundance and persistence of this shell has suggested the
distinguishing name for the beds in which it occurs. It is commonly
found in all the localities in which the zone is exposed. In most
eases the beds yielding it are coarse and friable, when the shells
are either fragmentary or rarely in good condition. The shells
figured from the Rhetic beds on the Continent are usually from beds
of sandstones, in which their casts only are preserved, which renders
their specific comparison with the sharply defined shells from Beer-
Crowcombe somewhat difficult.

The Avicula contorta from the latter place shows some variation,
the curved longitudinal ribs being much stronger and more inter-
rupted in some specimens than in others. I have also found the
shell in the thin band of clay resting on the Carboniferous Lime-
stone in the Vallis section, and also in the Bone-bed drift of the
same locality.

AvicuLA soriraRta, Moore. Pl. XV. fig. 11.

Shell convex, oblique, inequivalve, with eight regular radiating costa
passing from a very narrow convex umbone to the inferior margin ;
anterior auricle small; posterior auricle extended, ornamented with
very fine strize, and reaching to the inferior frontal margin.

* The figures given by Quenstedt in ‘ Der Jura,’ tab. 2. fig. 86-38, probably
belong to Lepidotus, and not to the genus Sargodon,

500 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

Only one example of this shell has been found. It is readily
distinguished from the A. contorta by its more produced posterior
auricle, by its less angular posterior side, by the coste being much
fewer in number, and by its narrower contour. Height 9 lines;
width 6 lines.

Loc. The “ Flinty bed,” Beer-Crowcombe.

Pracunopsis anpina. Pl. XVI. figs. 4, 5.

Anomia alpina, Winkler, Schicht. der Avic. contorta, pl. 1. fig. 1.
Anomia? Quenstedt, Der Jura, tab. 1. fig. 16.

Shell smooth, roundly ovate or orbicular, convex, variable ; umbo
with very slight ear-like expansion on the posterior side; ventral
margin and sides regularly rounded. Smaller valve flattened or
concave, rounded, closely fitting.

This shell appears to be identical with that figured by Quenstedt
above, which he doubtfully refers to Anomia. It is common in the
“« Flinty bed” at Beer-Croweombe, where species are found from 2
to 12 lines in length. In its more perfect state, when the shell
has the test preserved, the exterior is quite smooth; but when this
has been remoyed, the under surface exhibits, by aid of the lens,
numerous close-set longitudinal strie, which characterize the genus
Placunopsis, to which it therefore seems more nearly allied.

GERVILLIA PRacuRSOR. Pl. XV. figs. 6, 7.
Gervillia precursor, Quenstedt, Der Jura, tab. 1. figs. 8-11.

Shell smooth, oblique, elongated, convex ; hinge-line straight, pro-
duced posteriorly, bounded by a slightly raised horizontal rim;
umbones rather prominent, anterior ; ventral margin rounded; poste-
rior inferior margin angular. Right valve flatter than the left;
lines of growth distinct. The original pink colour of this shell is
shown by six or seven broadish longitudinal lines in two examples
in my possession.

Loc. From the “ Flinty bed” of Beer, where it is somewhat rare.

GERVILLIA oRNATA, Moore. Pl. XV. fig. 8.

Shell small, convex, elongated, tapering gradually to the apex;
hinge-line long, depressed, and slightly concave; the dorsal surface
possesses six or seven longitudinal ribs, which commence from the
umbo, and are extended to the ventral margin. These, as well as the
flattened area, are crossed by numerous lines of growth, and give
the shell a richly ornamented appearance.

Loc. This shell is associated with the Gervillia precursor in the
«‘ Flinty bed” at Beer. Three specimens only of the left valve are
known.

Length 4 lines; breadth 2 lines,

Lrva precursor. Pl. XY. fig. 9.
_ Lima precursor, Quenstedt, Der Jura, pl. 1. fig. 22-24.
Shell inequilateral, moderately convex, front rounded,apex narrow;

1861.] ~ MOORE—RHZTIC BEDS AND FOSSILS. 501

dorsal surface covered with very narrow, close-set, wavy strie, slightly
diverging outwardly, between which there are a multitude of minute
regular depressions.

The original figures given by Quenstedt appear to be casts; so
that close comparison is impossible. He intimates the possibility of
these Rheetic shells being the precursors of the Lima gigantea of
the Lias; but the Beer shells show the ornamentation of their sur-
faces to be different, and the Lima precursor to be a good species.
In the Z. gigantea, the longitudinal strize are broader and more
uncertain in their width than in the above shell, and the striz are
crossed by innumerable concentric raised lines, which are wanting
in the L. precursor.

When the test is perfect, this shell is nearly smooth (the ornamen-
tation only becoming visible on the worn specimens from the “ Flinty
bed” of Beer). It attains larger dimensions than the original figures,
Largest specimens, length 17 lines; breadth 12 lines.

OsTREA INTERSTRIATA. PI. XY. fig. 25,
Plicatula interstriata, Emmerich.

This is one of the most abundant shells in the Rheetic formation,
It characterizes the “‘ Ostrea-bed ” of the ‘“‘ White Lias ” in the sec-
tions given by Dr. Wright, at Garden Cliff, Wainlode Cliff, and in
Warwickshire. It occurs in the “ White Lias” of the West of
England, and is also especially abundant, both in the Vallis clay-
bed, and in the Mammal-drift near Frome. It is one of the most
characteristic fossils of certain of the Continental Rhetic zones.

OstTREA FIMBRIATA, Moore. Pl. XVI. fig. 24.

A species of Ostrea with a fimbriated margin is associated with
the O, interstriata in the blue clay-band at Vallis. It attains much
larger dimensions than the foregoing, but has hitherto only been
found in fragments.

Prcten Vatontensis, Defrance. Pl. XVI. fig. 6.

This shell occurs in the Rheetic beds in most localities. I have
obtained it from the ‘‘ White Lias” of Stoke St. Mary; in the
Avicula contorta zone at Uphill; and in the blue clay-band at
Vallis. It is usually in fragments or much crushed. Fragments
are also found in the Mammal-bearing drift of the same neighbour-
hood.

Azca Lycerri1, Moore. Pl. XVI. fig. 7.

Shell subrhomboidal, convex; umbones anterior, slightly depressed ;
dorsal surfaces of the valves in the young shell with fine close-set
strie, which in the adult are nearly obliterated by acute concentric
or transverse lines of growth, leaving the longitudinal strie scarcely
perceptible, except on the ventral margin and anterior end; anterior
side most convex, and rounding to the edge; posterior end depressed,
and separated from the side of the shell by an elevated indented rib,

502 PROCEEDINGS OF THE GEOLOGICAL SOCTETY. [May 22,

below which are three or four acute, indented, spreading coste. The
young shell possesses a sinus, commencing under the umbo and
widening to the ventral margin, which in the adult is less marked.
Obs. The area and the hinge-line of this beautiful species are not
clear of the matrix. It is very rare, and single valves only are
found. It is named after my friend Dr. Lycett, of Scarborough.
. Loe. From the “ Flinty bed” of Beer-Crowcombe. Professor
Suess has informed me that a somewhat similar shell is found in
Rheetic beds at Hirtemberg, south of Vienna.

Axtnvs, Sowerby.

Shells of this genus occur in the greatest abundance on the surfaces
of shelly layers of the ‘‘ Flinty bed ” at Beer-Croweombe. They pre-
sent considerable variety; so that were we disposed to multiply species,
many might be created. We propose, however, giving four well
marked forms, though probably even these may not be distinct
species, as passages between them might be established.

Few shells have been subject to greater transposition, or have
been placed under so many different genera, as those included in the
group under notice. Von Credner in ‘ Leonard und Bronn’s Jahrbuch’
1860, p. 307, remarks that one of the Rheetic species has by Roemer
been called Venus lassica, but without a figure; by Quenstedt in
‘Der Jura,’ Opis cloacinus; that Escher notices it, but without
naming it, from the Késsen beds; by Oppel and Suess it is called
Schizodus cloacinus ; and that it had previously been given by Borne-
mann, but without a figure, as Teniodon Hwaldi of Dunker.

In previous notices of the fossils from this zone, by Mr. Strickland,
the Rey. P. B. Brodie, and Dr. Wright, reference is made to a shell
called Pullastra arenicola, Strickl., which is said to occur very
abundantly, but only in casts, and of which no figure has been given :
there is no doubt it belongs to the group under consideration. Similar
shells have also been included by other English authors under the
genera of Tellinites, Isocardia, ‘Cucullea, Donac, Sedgwickia, and
Sch izodus.

It is not clear wherein the following shells from Beer differ from the
Axinusof Sowerby; and his name, haying priority,is therefore retained.

Axtnvs ctoacinus. Pl. XV. fig. 16.
Opis cloacinus, Quenstedt, Der Jura, tab. 1. fig. 35.

Shell triangular, quite smooth or with very delicate transverse
strie, broader than long, convex ; umbones slightly anterior ; anterior
end rounded ; posterior end slightly extended, divided from the dorsal
surface by a depressed ridge running from the umbo to the posterior
ventral margin; beyond this ridge is an obtuse angulated area.

This is the most abundant of this group of shells, and its charae-
ters appear to be persistent. It is more equilateral than the other
forms accompanying it, and answers to the figure given of Opis cloa-
cinus in Quenstedt’s ‘ Der Jura’*. In the best-preserved specimens

* This shell also resembles the Myophoria of Merian in Escher’s Vorarlb.

Pl. iv. fig. 42.

1861.) MOORE—RHZETIC BEDS AND FOSSILS, 503

the exterior is covered with a bluish or cream-coloured enamelled
surface, the transverse strie being exhibited only on the more worn
examples. Width 7 lines; length 5 lines.

Locality. The “ Flinty bed” of Beer-Crowcombe.

Axrnvs pepressus, Moore. Pl. XV. fig. 17.

Shell flattened, convex, transversely oval, nearly smooth or with
distant transverse lines of growth, inequilateral ; umbones depressed,
slightly anterior; posterior and anterior ends towards the ventral
margin somewhat rounded.

This shell is much flatter than the A. cloacinus, and its form gene-
rally more rounded; and, whilst the latter possesses a decided poste-
rior ridge and acute area, in the A. depressus they are more rudi-
mentary, or with but a slight thinning out of the valve towards the
posterior edge. Length 54 lines; breadth 9 lines.

Axtnvs concentricus, Moore. Pl. XY. fig. 19-21.

Shell rather small, transverse, ovate, flattened, inequilateral ;
umbones convex, anterior; posterior end produced, with a slight
ridge and flattened area, which commence from the umbo; ventral
margin and anterior side rounded; dorsal surface with numerous
regular or widely separated concentric lines of growth, which
obliquely cross the area.

Quenstedt, in ‘ Der Jura,’ tab. 1., gives some bivalves of uncertain
forms. His figures 28 & 30 in all probability represent the above
species.

Locality. tis common in the “ Flinty bed’ of Beer. Largest ex-
ample, length 4 lines; breadth 5 lines.

Axinvs ELonGATUS, Moore. Pl. XV. fig. 18.

Shell originally smooth, equivalve, inequilateral, convex ; umbones
anterior; dorsal surface covered with very fine, close-set, regular,
transverse striz ; anterior side rounded ; posterior side flattened and
produced, and tapering to the ventral surface.

This shell is to be distinguished from those previously described
by its more transverse elongation, by the finer and more regular
strie on its surface, and by its being more inequilateral. Two
examples only of this genus, belonging to the above species, with
both valves, are in my possession. Height 3 lines; breadth
5 lines.

Locality. From the “ Flinty bed” of Beer-Crowcombe.

PLEUDROPHORUS ELONGATUS, Moore. Pl. XV. figs. 14, 15.

Shell ovately oblong, depressed, most convex at the umbones,
which are very anterior ; anterior end roundly tapering, posterior
end flattened, angular; from the umbones a ridge crosses the valve
to the posterior ventral end, behind which is an angulated area; a
second more depressed ridge separates this from a lengthened flat-
tened dorsal margin. The front of the shell possesses lines of

504 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

growth, which cross the ridges at right angles, and return obliquely
on the dorsal side towards the umbones,

Examples in our possession present considerable variety, depending
on the more or less worn condition of the test. In some the lines
are very acute, whilst in others the shell has a much smoother
surface.

Under the name of Cypricardia Suevica, a shell is figured by Oppel
and Suess in “ Kossener Schichten,”’ table 1, fig. 4, from Niirtingen,
which, though apparently distinct from our species, probably belongs
to the same genus.

Hitherto the genus has not been recognized higher than the Per-
mian beds.

Locality. The “ Flinty bed” of Beer-Crowcombe. Perfect speci-
mens are rare, Length of largest examples 18 lines ; depth 7 lines.

PLEUROPORUS ANGULATUS, Moore, Pl. XY. figs. 12, 13.

Shell rather small, inequivalye ; umbones small, depressed, ante-
rior; anterior end angular; posterior end deepest, flattened, and
slightly angular; dorsal surface of perfect shell quite smooth,
crossed by three acute, slightly curved ribs passing from the um-
bones to the posterior ventral margin.

This species is rare. It may readily be distinguished from the
P. elongatus by its very obtuse form, and by its generally smoother
surface. Length 8 lines; depth 44.

Locality. The “ Flinty bed,” Beer-Crowcombe.

Carpium Ruzricum. Pl. XV. fig. 28,
Cardium Rheticum, Merian, Escher’s Vorarlb. pl. 6, fig. 40, 41,

Shell nearly smooth, globose, convex, nearly equilateral ; umbones
prominent, beak recurved ; posterior and anterior sides rounded ;
ventral margin round and slightly extended; posterior end with
numerous depressed longitudinal ribs; dorsal surface either quite
smooth or crossed by very numerous faint concentric strie, which
decussate the longitudinal ribs on the posterior side.

This shell appears to have been quite smooth in its more perfect
condition, and only shows the striz on its dorsal surface in speci-
mens that are more or less worn. Length 7 lines; breadth 8 lines,

Locality.—The “ Flinty bed” of Beer, where it is somewhat rare.

Lepa Tire, Moore. Pl. XV. fig. 25.

Shell oblong, equivalve, rather inequilateral, convex, inflated,
thick ; umbones closely incurved over a concave oblong area; mar-
gins of the valves close-set and smooth ; ventral margin and ante-
rior side rounded; posterior end produced; exterior of the valves
covered with very fine, regular, concentric, transverse striz.

I have but one example of the above shell ; but this is fortunately
in very good condition, and is one of only three instances from Beer
in which both valves of the shell are attached. Oppel and Suess in
«‘ Késsener Schichten,” tab. 2. fig. 9, have giyen a shell under

1861. ] MOORE—-RHETIC BEDS AND FOSSILS. 505

the name of Leda Deffneri (the Leda alpina in Winkler, pl. 1. fig. 8).
The shell figured by these authors differs materially from the Leda
Titei. The umbones of the former are more anterior; the posterior
side is angular and more attenuated; and the concentric striations
altogether differ. Indeed, as far as I can judge by the figures of
these authors, their shells represent, not the genus Leda, but that
variety of the Awinus which I have given under the name of the
Axinus elongatus (Pl. XV. fig. 20).

It is named after my friend Wm. Tite, Esq., M.P., F.R.S., F.G.S.

Locality. Beer-Crowecombe. Height 4} lines; breadth 8 lines.

Moprora mint, Sow. Pl. XY. figs. 26 & 27.
Mytilus minutus, Goldfuss, Petref. ii. p. 173, pl. 180, fig. 6.

Shell elliptical, convex, smooth or with concentric irregular
striations; umbones thick and blunted, subterminal; hinge-line
straightened ; upper portion of the dorsal surface much convex, and
flattening to the central margin, which is rounded.

This shell is one of the most abundant in the “ Flinty bed” at
Beer-Crowcombe, and is also common in the ‘‘ White Lias ” in many
localities in the West of England. It is also one of the most cha-
racteristic shells of the Rhetic sandstones of Suevia. It presents
considerable varieties in form, some being thinner and more elongated
than others. In its young state it is very obtuse and convex. They
occur at Beer from 2 lines in length by 14 line in height, to 20 lines
in length, and 10 lines in height in adult examples,

Prrromya, Moore, 1861.

Shell oblong, thin, smooth, convex but depressed, inequivalve, in-
equilateral; umbones anterior, depressed, and curving to the ante-
rior side; dorsal margin extended, slightly rounding or acute; ven-
tral margin rounded; anterior side most convex; posterior side
flattened, concave, curved, widely gaping. Dorsal surface covered
with strong transverse concentric or wavy lines of growth, which
on the right valve continue to the posterior edge. On the left valve
these are interrupted on the posterior side by a ridge, passing from
the umbo to the posterior ventral margin, beyond which the shell
is extended into a flattened or concave winged area, with a rounded
or angular margin at the ventral extremity.

We are not aware that the inequivalve character in the genus
proposed above is so largely possessed by any other of the Myade,
to which family it evidently belongs. All the shells in my posses-
sion are single valyes, and none have the interior or the hinge
exposed. or some time we were disposed to consider that valves
haying so different a character were to be referred to more than one
species; and it was not until after an examination of many examples
that a satisfactory determination was arrived at respecting them ;
it was then found in every instance that no right valve possessed
the ridge and extended area, which are present invariably on the
left. In other respects the valves are precisely similar.

506 PROCEEDINGS OF THE GEOLOGICAL socreTy. {May 22,

PreromyA CrowcomBetA, Moore. Pl. XY. figs. 22 & 28.

Shell thin, smooth, inequilateral, inequivalve, ovately oblong, con-
vex but depressed; anterior end most convex, rounded; posterior
side depressed or slightly concave, rismg again towards the edge,
gaping ; surface of the valves either nearly smooth or with waved
transverse lines of growth, continued on the right valve to both
extremities ; posterior side of the left valve possesses a slightly
curved depressed ridge, passing from the umbo to the ventral mar-
gin, beyond which the shell is extended into a winged, flattened or
slightly concave area.

This shell is abundant; and in all the examples I have seen,
the right valve is without the posterior ridges and area, which are
invariably present on the left. Some of the shells have a grey ena-
melled exterior, in which state they are almost smooth. When this
is abraded, the transverse strize are most visible. Height 7 lines;
breadth 12 lines,

Locality. The ‘ Flinty bed” of Beer-Crowcombe.

Preromya stuetEx, Moore. Pl. XY. fig. 24.

Shell nearly smooth, inequilateral, oblong, convex ; posterior side
flattened, ridge acute, anterior moderately convex ; transverse lines
of growth on dorsal surface.

This shell differs from the P. Crowcombeia in being more regularly
convex, and in its straighter and more symmetrical form. Only the
left valve of this species is known.

Locality. Found in the “ Flinty bed” with the P. Crowcombeca, at
Beer.

MYACcITES sTRIATO-GRANULATA, Moore. Pl. XVI. fig. 1

Shell ovately oblong, twice as wide as long, inequilateral, convex ;
umbones rather anterior; anterior end slightly depressed, and side
rounded; posterior side extended, graduating to a rounded edge;
dorsal surface covered by a thin grey test, in which are situated
innumerable minute rounded eranulations, arranged in close-set
longitudinal lines, most prominent on the anterior side; these are
crossed, especially towards the ventral margin, by numerous fine
transverse lines of growth.

Only one specimen of the above shell has been found. Width
20 lines ; length 10 lines.

Locality. The « Flinty bed,” Beer-Crowcombe.

Although it will be seen ‘that there are several species of the
family of Myade from the Beer bed, specimens are by no means
numerous. When studying these shells it is of importance to
attend to their external condition, without which specific forms
might be multiplied. Were the thin outer integuments in the above
shell abraded, its granulated character would ‘disappear, leaving it
either nearly smooth or exhibiting only its transverse lines of
growth, such as are seen on the Anatina precursor, Quenst. (‘ Der
Jura,’ pl. 1. fig. 32.) I am disposed to believe that if the latter
shell, together with the A, Swessi?, Oppel, found in the Rheetic

1861. ] M0ORE—RH#TIC BEDS AND FOSSILS. 507

beds, had possessed their tests, they would have to be removed from
Anatina to Myacites. Both species are given below, but are not in
a condition to establish this point.

AwnatTiIna? pR=cURSOR, Quenstedt. Pl. XVI. fig. 3.

Shell transversely oblong, subtriangular or ovate, convex, inequi-
lateral; anterior side rounded, depressed; posterior end extended ;
umbones rather anterior, depressed; transverse lines of growth on
dorsal surface distinct, curving round a slight area on the posterior
dorsal margin.

It is not improbable that this shell may hereafter be found to
possess a granulated exterior ; but the surface of the test is removed
in the examples in my collection. As it does not possess the cha-
racters of the genus Anatina, and also differs in shape, it may have
to be removed to Myacites. Width 14 lines; height 7 lines.

Locality. From the “ Flinty bed” of Beer-Crowcombe.

Awnatina? Svxssr, Oppel. Pl. XVI. fig. 2.

Shell ovately oblong, conical, twice as wide as long, inequilateral ;
umbones anterior, slightly depressed; anterior end rounded; poste-
rior side flattened, edge rounded, slightly curving upwards ; frontal
margin of shell concave; a very slight ridge from the umbo crosses
the shell obliquely, dividing it into two nearly equal portions. The
surface is covered by concentric striations, which on the posterior
side curve upwards.

This shell somewhat differs from the figure given by Dr. Oppel;
but there cannot be a doubt that it belongs to the same species.
That gentleman remarks that the species is found with the Anatina
precursor in the sandstone about 8 feet below the Bone-bed at
Nirtingen. In my example the outer integument is removed ; and
therefore the precise character of the exterior may not be given in
the figure. Like the last-named} shell it may eventually have to be
referred to Myacites. Width 16 lines; height 8 lines.

Locality. From the “ Flinty bed”’ of Beer-Crowcombe.

Myornorta postera, Bronn. Pl. XVI. figs. 8-10.
Trigoma postera, Quenstedt.

Perfect shell quite smooth, trigonal, convex ; anterior and ventral
margins slightly rounded; umbones rather depressed, directed ante-
riorly ; area broad, and often very acute, with about twenty longi-
tudinally curved, somewhat variable coste; dorsal surface smooth
when perfect, when worn presenting numerous regular concentric
transyerse ribs, which in some examples cross the marginal carina,
when it is distinctly denticulated. In the left valve the carina is
distinct and single, either smooth or denticulated, and widening to
the frontal margin. In the right valve the shell possesses two or
more carin, separated by smooth longitudinal sulcations.

From the above remarks it will be seen that, like many others
of the family, this shell presents considerable variety, which in this
case does not appear to be due to age. Attention is also neces-

508 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. (May 22,

sary to the condition in which the shells are found; for in many
of the Beer specimens the outer surfaces of the shells are pre-
served. ‘They are then seen to have perfectly smooth exteriors,
whilst when this has been eroded or has perished the transverse
strie on the dorsal surfaces are perceptible. Without attention to
this fact several species might be created from what are only vari-
eties or different conditions of the same shell. The areas in the MZ.
postera are much more acute in some examples than in others, but
they all possess, though with some little modification, longitudinal
strice of the same general character. ‘The transverse striew on the
dorsal surface amount to upwards of fifty in number. Height of
shell 5 lines; breadth 53 lines.

Locality. From the “ Flinty bed” of Beer, where it is not un-
common.

CrrirHiuM constrictum, Moore. Pl. XVI. fig. 13.

Shell small, narrow, elongated, tapering, apex rather obtuse ;
volutions six or seven, each ornamented with three prominent equi-
distant transverse ribs, volutions separated by a deep angular con-
cavity.

Observations. This is a pretty and well-distinguished species.
Between the ribs there are indications of slight longitudinal striz.
The aperture appears to have been rounded, but is imperfectly dis-
closed. Itis very rare. Length 3 lines; width 3 of a line.

Locality. The “ Flinty bed”’ of Beer.

CreriruiumM pecorarumM, Moore. Pl. XVI. fig. 14.

Shell small, turreted, tapering, reticulated ; volutions eight or nine,
conical, with encircling prominent ribs; sutures concave, angular ;
oblique longitudinal striz cross the ribs, and, passing into the angles
of the sutures, give the shell a generally reticulated aspect.

Of this shell I have only two examples. Length 3 lines; breadth
1 line.

Locality. The “ Flinty bed” of Beer.

Crritaium cytinpricum, Moore. Pl. XVI. fig. 15.

Shell small, very slender, regularly tapering ; volutions ten, orna-
mented with three transverse slightly oblique ribs, volutions rather
distant, with a somewhat rounded concave suture.

This shell is very rare, and is to be distinguished from the C.
constrictum by its more elongated and cylindrical form, the whorls in-
creasing very slowly in size, and also by its less angular and rounded
sutures. Length 23 lines; width 3 a line.

Locality. The “ Flinty bed ” of Beer.

Crerrru1um Ruzricum, Moore. Pl. XVI. fig. 16.

Shell small, tapering; volutions seven or eight, flattened, with
encircling strie, the coarsest of which are situate over the sutures,
which are slightly concave.

This shell differs from those previously described, by the more

1861. ] -MOORE—RH ATIC BEDS AND FOSSILS. 509

flattened surface of the whorls, which have a greater number of en-

circling ribs, and by its possessing one or more depressed ribs which

pass into and divide the suture. Height 3 lines; breadth ? line.
Locality. The “ Flinty bed” of Beer.

CYLINDRITES FusIFoRMIS, Moore. Pl. XVI. fig. 18.

Shell very small, smooth, apex acute, with four rather oblique
volutions, the upper ones flattened; the last whorl more convex and
ovate, and tapering at its base into an extended folded columella.
Aperture longitudinallyoval. Length 14line; width 4 line. Three spe-
cimens of this shell are in my cabinet from the “ Flinty bed”’ of Beer.

All the species of this genus at Beer are very minute. Some casts
of larger size have been found in the Rhetic beds of Suevia; and
M. Merian mentions a species from the beds of Vorarlberg.

Criinprites ovyatis, Moore. Pl. XVI, fig. 19.

Shell small, smooth, longitudinally ovate, apex acute; whorls five,
regularly tapering and slightly convex, terminal whorl large and
convex. A slight ridge encircles the upper portion of the whorl.
Lines of growth are perceptible on the last volution. Aperture
narrow at the top, but expanding at the base. Only one specimen
of this shell is known. Length 4 lines; breadth 2 lines.

Locality. The “ Flinty bed” at Beer.

CyLinprites ELoneGatus, Moore. Pl. XVI. fig. 20.

Shell smooth, elongate, cylindrical ; whorls five, the upper convex,
spiral, and divided by a narrow rounded suture. The terminal whorl
is quite cylindrical and occupies nearly four-fifths of the entire length
of the shell. Aperture not exposed.

Only one specimen of this species has yet been found. Its length
is 23 lines; breadth 1 line. It appears very similar in form, though
smaller, to a cast figured in ‘ Kossener Schichten’ (tab. 1. fig. 1), by
Oppel and Suess, under the name Acteonina, sp.

Locahty. From the “ Flinty bed” of Beer.

CYLINDRITES OvIFoRMIS, Moore. Pl. XVI. fig. 21.

Shell very small, smooth, elongate, cylindrical ; whorls four, with
a very depressed spire; apex rather acute. ‘The terminal whorl is
cylindrical, occupying the greater length of the shell, and at its
base is folded and slightly tapering.

This shell differs from the C. elongatus chiefly in the more depressed
character of the upper whorls, and in its more tapering base. Length
23 lines, breadth 1 line. Aperture the length of the last whorl, and
very narrow.

Locality. The “ Flinty bed,” Beer-Crowcombe.

Cuemyitzia Henrict? Pl. XVI. fig. 12.
Cerithium Henrici? (Martin), Mém. Soc. Géol., 2 sér. vol. vi. pl. 2.
fig. 17, 18.

Shell small, tapering, thick ; volutions six or seven, conical, narrow,
with rather oblique or curved longitudinal prominent coste ; sutures
slightly concave and rounded; aperture slightly extended.

VOL, XVIJ.—PARI I. 2M

510 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

I have but one adult example of this shell, and this has lost a
small part of its apical portion. The terminal whorl is rather more
conical and ovate, and its strie, which are about sixteen in number,
are less prominent than on the preceding whorls. This shell is in
height 3 lines; in breadth 1 line. It is, with some doubt, referred
to the Cerithium Henrici of Martin, though it seems rather thinner.

I am possessed of another very small Rissoa-looking shell with
four whorls, which may probably be its younger form.

Locality. The “‘ Flinty bed” at Beer.

Cuemnitzia niTIDA, Moore. Pl. XVI. fig. 11.

Shell small, smooth, turreted, spire rather obtuse, with five slightly
oblique, rounded or convex vyolutions, separated by a well-defined
suture.

We have obtained only one example of this shell. Dunker
figures a Rheetic shell under the name of Paludina solidula, which
appears to be similar to it. Unfortunately, as is the case with most
of the Rhetic shells from Beer, the aperture is not exposed, and
therefore does not help to a generic determination ; but, as the whorls
of the above shell on close examination present a tendency to be
slightly costated, we are induced to place it under the above genus.
Length 23 lines; breadth 1 line.

Locality. The * Flinty bed,” Beer.

Natica Oppretit, Moore. Pl. XVI. fig. 17.

Shell small, smooth, glossy, globose; whorls four, convex; spire
depressed ; apex acute; the last whorl much increased in size, and
showing lines of growth; umbilicus small; aperture large, ovate.

This is the only Natica yet found in this zone in England. It
probably represents a cast given by Oppel and Suess in ‘ Kossener
Schichten,’ tab. 1. figs. 3a, 36, and also by Quenstedt in ‘ Der Jura,’
tab. 1. figs. 17-20, though our shell does not attain so large a size.
The former authors give figures of a still larger species, which, from
the casts, must haye possessed more angular volutions. Natica
alpina, Merian, is also from Rheetic beds, but is different from our
shell. It is the most common Gasteropod in the “ Flinty bed” at Beer-
Crowcombe, and is named after my friend Dr. Oppel of Munich.

Trocuvus Wartonn, Moore. Pl. XVI. fig. 23.

Shell small, conical, obtuse; whorls four or five, flattened or
slightly convex, covered with very fine transverse striz; aperture
oblique, depressed ; umbilicus small; base flattened or slightly con-
cave, with five encircling strie.

In its young state this shell is abundant; but the more adult
forms are not so. When young it is more depressed, and the striz
are more strongly marked.

The species, from the “ Flinty bed”’ at Beer, is named after my
friend Wm. Walton, Esq. of Bath.

Trocuvs nupus, Moore. Pl. XVI. fig. 22.

Shell small, conical, quite smooth, strie obtuse ; volutions four or
five, slightly oblique, smooth, separated by a slightly oblique rounded

1861.] MOORE—RHZETIC BEDS AND FOSSILS. oll

suture; base smooth, moderately concave; mouth depressed,
oblique.

This species is found with the 7. Waltonz, but is more rare, and
is well distinguished from it by the above characters.

Locality. The “ Flinty bed,” at Beer.

Srraparotus Surssit, Moore. Pl. XIV. figs. 2-5.

Shell small, discoidal, depressed, thickest at the back; whorls
flattening towards the umbilicus, and increasing very slowly without
change of form or ornamentation, the last whorl possessing about
sixteen tubercles situate close upon the back, each continuing into
a broad depressed rib, terminating in a small lengthened tubercle
over the umbilicus, with slight concave depressions between the
ribs. By aid of the lens very fine striz may be discovered which
are crossed by equally fine longitudinal lines, giving the shell a
slightly reticulated aspect. Under side somewhat concave, with
ornamentation less defined. Back of the shell flattened, with three
equally raised ridges, situate between two lateral, less elevated
tubercular ridges ; between the ridges are four smooth longitudinal
grooves.

I was at first disposed to consider this little shell an Ammonite ;
but, as a trifling difference is apparent on the sides, and also a very
slight concavity on the under side, this is rendered doubtful. With
some hesitation it is placed under the above genus. Only one spe-
cimen has hitherto been obtained. It is named after my esteemed
friend Professor EH. Suess, of the Imperial Museum of Vienna, who
has given much attention to the fauna of the Rhetic Beds.

Height of the shell 4 lines ; width 5 lines.

Loc. The “ Flinty bed,” Beer-Crowcombe.

Curton Ruzticus, Moore. Pl. XVI. figs. 28, 29.

Plate small,smooth, elongately ovate, rounded; umbo elevated, with
a broad sinus; lateral areas extended and depressed, with irregular
concentric lines of growth.

Numerous valves or plates of the above little species occur in the
blue clay-bed at Vallis. The largest example measures 33 lines in
breadth by 2 lines in depth.

Zoophyton.
MonvTLivaLtia.

This genus is represented in the ‘‘ Flinty bed” at Beer by a
single specimen. It has been placed in the hands of Mr. Tomes for
description in his paper on new Liassic Zoophytes. He reports to
me respecting it, that it is “a horizontal section, near to the calices,
probably of some species of Montlivaltia. The septa are remarkably
thin, and their sides appear to be without tubercles. Fine cycla
are traceable, none of which appear to have met in the centre; and
hence it is probable that in this species there was no spurious colu-
mella, which is so often seen in this genus. It must, however, be
remembered that this may depend in some measure upon the age of
the specimen.”

2mu 2

512 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

Echinodermata.

Numerous fragmentary remains of this family, chiefly spines, are
to be found in the “ White Lias ” of Stoke, &c., on the surface of the
“Flinty bed” at Beer, and in the blue clay at Vallis. Dr. Wright.
enumerates four species from the ‘‘ White Lias” of Pinhay Bay—viz.
Cidaris Edwardsii, Wright, Pseudo-diadema lobatum, Wright, Hemi-
pedina Bechet, Broderip, H. Bowerbanku, Wright,—which, if from
the true ‘‘ White Lias,”’ we should consider Rheetic species.

Ophiura?
A single joint found in the clay-band at Vallis appears to have
represented this or an allied genus in the Rhettic age.

Encrinite.

Joints of a very small Encrinite are not uncommon in the blue
marl at Vallis.
Cirriped.
Poxiicires Ruzxricus, Moore. Pl. XVI. fig. 30.

Valves small, enamelled, elongated, triangular, pointed at the
upper end; an elevated central ridge divides the valves longitudi-
nally, on either side of which are very fine longitudinal stric, which
are crossed by transverse lines of growth, giving the valve a richly
ornamented appearance. Length 13 line; breadth 13.

Though generally imperfect, the shell is not uncommon in the
blue clay resting upon the Carboniferous Limestone in the Vallis
section. It is at present the oldest known representative of the
family Cirripedia.

Entomostraca.
Cypris tiassica (?), Brodie.

The upper surfaces of the blocks of “ White Lias” in the sec-
tions near Taunton are frequently covered with the shells of this
little Crustacean. The same conditions prevailed when the ‘ Flinty
bed’ at Beer-Crowcombe was deposited, as the shells are very nu-
merous on its weathered surface. In the Vallis section it is very
rare, and only represented by a single specimen attached to a frag-
ment of Lima precursor.

EstHerta minuta, Alberti, sp.
Posidonomya minutia, Auct.

At the Vallis, near Frome, a few specimens of this little crustacean

occur in a cream-coloured limestone, and also in the conglomerate.
Plants.
NaTapITA AcumINaTA (?), Buckman, Geol. Cheltenham, p. 93.

Two little groups of Plants, apparently identical with the above,
have been found in the thin layers of stone interposed between the
Conglomerate and the Inferior Oolite at Vallis, associated with
examples of Estheria and Insects.

The stone is concretionary, and lithologically similar to the “‘ White
Lias,”’ or to the ‘‘ Landscape-stone ;’”’ and I am therefore disposed to
consider it to be on the same horizon as the Cypris- and Plant-bed

|
|

Mam Aue.
Microlestes antiquus......... Plioning ews ee eee ce ae Holwell.
Pisces.
Sargodon tomicus............ Quenstedt ./Pl. XV. fig.1. ...._Beer, Holwell.
WeScual orataiescsecn eens: Riley: GoaS tiie aceuaaees seneccue ‘Beer, Vallis, Holwell.
Weprdotusiteeth ote rs ee spices isseniossas ceases Manas se aeatamaneee (Beer, Vallis, Holwell.
| Saurichthys acuminatus .../Agassiz ...|..........ssssccesseeees ‘Beer, Holwell.
VOCS cceeconcduadosoaee PAD ASSIZ i stee |eceenepeee actions (Beer, Vallis, Holwell.
Acrodus minimus......;..... ING ASSIZ sel esoncnectenmenseascster ‘Beer, Vallis, Holwell.
Gy role pis scalespoutean ne only tater aqua. calschcesnancamar eecee anne Beer, Vallis, Holwell.
Mo.uuuvsca.
Avicula contorta ............ Portlock ...|Pl. XV. fig. 10. Beer, Vallis, &c. &c. |
solitaria” <24.2-c---eees Moore ...... Pl. XV. fig. 11. | Beer.
Anatina precursor ......... Quenstedt .|/Pl. XVI. fig. 3. Beer.
PINGS Gaenaedneseaeaosac Oppelieae Pl. XVI. fig. 2. Beer.
aren Noy Cebtitee-ceenseree eae Moore ...... Pl. XVI. fig.7. _|Beer.
| Axinus cloacinus ............ Oppel & 8. |Pl. XV. fig. 16. ‘Beer.
—— depressus .,............. Moore ...... Pl. XV. fig. 17. | Beer.
concentricus ............ Moore ...... Pl. XV. figs. 19-21. Beer.
ClON SAIS ere saeeereere (Moore ...... Pl. XV. fig. 18. Beer.
Cardium Rheeticum ......... (Merian...... Pl. XV. fig. 28. Beer.

1861. ]- MOORE—RHETIC BEDS AND FOSSILS. 513

of the Rey. P. B. Brodie, noticed in his work on Fossil Insects. The
conglomerate separates it from the band of blue clay containing the
Avicula contorta, and the fish- and other remains previously noticed.

Carabide.

A few wings of Coleopterous insects occurring with the Hstheria and
Plants previously mentioned, appear closely allied to the Carabidae.

It will be seen, from the foregoing organic remains, that the beds
we propose including in the Rhetic formation, embracing the “‘ White
Lias ”’ and those which in this country are between it and the Keuper
Sandstones, yield an interesting and peculiar fauna, differing in its
general facies from that found in the Lower Lias above, and entirely
from that in the Keuper Sandstones below; whilst it also differs
from that in the St. Cassian stage, which follows the Rhetic forma-
tion on the Continent.

On another occasion I hope to be able to make Emporia additions
to the Mammalia, Reptilia, and Fishes of this zone ; but, without in-
cluding these families, I have shown that the Mollusca, Crustacea, dc.
amount to at least fifty-two species,—some of the genera, such as.
Chiton, Pollicipes, and Pteromya, being recognized in it for the first
time ; and this list I have no doubt may be increased hereafter.

Dr. Oppel, in ‘ Kossener Schichten,’ states that, on the whole, but
twenty-five species have been found in this zone abroad. Of these,
fourteen species at most are all we are enabled to identify with
British species.

Table of British “ Rhetic”’ Fossils, from the Avicula contorta zone,
noticed in this Paper.

Genera and Species. | Authority Reference. Locality. |

514

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

[May 22,

Table of British “ Rhetic” Fossils, from the Avicula contorta zone
(continued).

| Genera and Species.

Authority.

Motuuvsca.
Discina Townshendii ...... Davidson...
Gervillia precursor . ....... Quenstedt
—— OFNALA ...eeeeeceeeeeeeee Moore ......
Lima precursor ............ Quenstedt
Medal ite as. cescewsnsuaee ses Moore ......
Modiola minima ............ Sowerby
Myacites striato-granulata .|Moore ......
Myophoria postera ......... Quenstedt
Ostrea fimbriata ............ Moore ......
interstriata ~.2.0.0...>. Emmerich
Pleurophorus angulatus ...|Moore ......
elongatus ............04. Moore ......
Placunopsis alpina ......... Winkler
Pteromya Crowcombeia ...|Moore... ...
RUT SG eaocoganS4adoagnaae Moore ......
Pecten Valoniensis .........! Defrance ..
Bivalves, uncertain’ ....2...:|..-...<ec«s+ecs
Straparolus Suessil .........|Moore ......
Trochus mugusyssceesse seers: Moore ......
Wraltoniigesssse ees Moore ......
Chemnitzia nitida............ Moore ......
Cerithium Henrici?.........) Martin
— constrictum ............ Moore ......
—— decoratum..............- Moore ......
—— cylindricum ............ Moore ......
Rhzeticum...............| Moore ......!
Chiton Rheeticus ............ Moore ......
Cylindrites fusiformis ...... (Moore ......
OVALISS petesainn sackiaceee Moore ......
elongatus ............... Moore ......
OvlOnmismcansscesseeess Moore ......
Natica Oppelii ait sin Upinlelniasiate's Moore ...... |
PLanra.
Naiadita acuminata .........| Buckman
CRUSTACEA.
Cypris liassica ............... Brodie ......
Hstheria minuta ............ Alberti......
CrrRIPEDON.
Pollicipes Rheeticus .........) Moore ......
EcHINODERMATA.
Hichini; ispiness;Q0: | accacincccleceetne eee.
Ophiura;?-jomts Of). -.c0scs|eeee ease ceee
Encrinites, stems of ....,...-}.....e..c+.-s0
ZOOPHYTUM.
| Montlivaltia 22ett-...-cccosn}eeece se eaest-
INSECTA.
Carabidse? wingsiof .:-0.0).|Saeceeeats ss -e
ANNELIDE.
Serpula, traces of ............!.....--

Reference. Locality.
bononsbocantenasdaaoboue Beer.
Pl. XV. figs. 6, 7. |Beer.
Pl. XV. fig. 8. Beer.
MIBIEexeye fig 9. Beer.
Pl. XV. fig. 25. |Beer.
..|P1. XV. figs.26,27. |Beer, &c.
Pl. XVI. fig. 1. |Beer.
Pl. XVI.figs.8-10. |Beer.
Pl. XVI. fig. 24. |Vallis.
Pl. XVI. fig. 25. |Vallis, Stoke, &c. &e.
Pl. XV.figs.12,13. |Beer.
Pl. XV.figs.14,15. |Beer.
. XVI. figs. 4, 5.|Beer.
Pl. XV. figs.22,23. |Beer.
Pl. XV. fig. 24. | Beer. [&e.
|Pl. XVI. fig. 6. |Vallis, Uphill, Stoke,
Pl. XVI. figs.26, 27.|Beer.
Pl. XV. figs. 2-5. |Beer.
Pl. XVI. fig. 22. |Beer.
Pl. XVI. fig. 23. |Beer.
Pl. XVI. fig. 11. Beer.
XVI. fig. 12. |Beer.
Pl. XVI. fig. 13. |[Beer.
Pl. XVI. fig. 14. |Beer.
IL Qvale fg. 15. |Beer.
Pl. XVI. fig. 16. |Beer.
Pl. XVL figs. 28,29. Valls.
Pl. XVI. fig. 18. |Beer.
Pl. XVI. fig. 19. Beer.
Pl. XVI. fig. 20. |Beer.
Pl. XVI. fig. 21. Beer.
Pl. XVI. fig. 17. Beer.
iikgcisdeaaiecesteanieouer Vallis.
Mata dete mewn shea Beer, Stoke, Vallis, &c.
ReeScodococondabagacdod: Vallis.
Pl. XVI. fig. 31. Vallis.
PEACE OCOD TOI cO nnn Vallis, Stoke, Beer, &c.
BRED anacnanincoehocnne Vallis.
Selene abel ceeeeesaeeeee Vallis.
is sias sa bineeeheaaee meee Beer.
sia'sn oe ewrabaeee Don ae eee Vallis.
..|Beer.

eeee
2 AS ee eee

1861. | MOORE—RHZ£TIC BEDS AND FOSSILS. 515

APPENDIX.

Section at Shepton-Mallet.—Whilst this paper has been going
through the press, I have made an excursion along the unfinished line
of Railway from Shepton-Mallet to Wells. In doing this I was much
gratified to find that an admirable section of the Rheetic beds has
been opened up, in which all the strata from the Red Keuper Marls
to the Ammonites Bucklandi beds are exposed. ‘There is probably
no other section in this country in which continuously, and at one
view, these zones of rock can be so well studied; and fortunately
there is every probability that the sides of the railway-cutting at
this point will always remain open. The section given below is
about a mile west of Shepton-Mallet; the beds have a gradual dip
to the east towards that town.

Section at Shepton-Mallet (in ascending order).

ft. in.
1. Red Keuper Marl............ 10 0} 14. Blue stone .................006
2; Yellowish sand’ .....¢......... 1 0/15. Blue stone ....
3. Green sandstone ............ I Gas (Olen oponeacdeopedoes
PIG lstvane ss Peneece et vaciscaces eines OPP ELCG SIRO) nandosansonsunoanuonsodesee
5. Green sandstone ............ 2 0/18. Dense black clay ............ 12 0
6. Green sandstone .. ......... On Onto lintyabed: seeectece eter tac 1 0
Tos CHES Neca he aneceeeanee apr anee Ora) 20 Bluetclaygynseecssscosostee 2 6
8. Yellowish sandstone ......... 0 921. “ White Lias ;” about twenty beds ;
SMU LAV ito ict. ceteb tc cecser cise see 0 2 passing upwards into thin and
10. Yellowish sandstone ......... 0 6 somewhat irregular beds repre-
Wie Greenishtclayernscc2.c. deco: 0 5 senting the Saurian and other
12. Yellow sandstone ............ 1 0 zones at Beer-Crowcombe and
ese TUCICLA Ya wrote: choices ses 120 Street.

The sandstones Nos. 3 to 14, which are superimposed upon the
Red Marls, would yield very excellent building-stone, could they be
extracted over any considerable area. They are apparently destitute
of organic remains, though they contain the black vegetable-like
patches noticed in the same zone at Beer-Crowcombe: what these
are derived from, it is difficult to conjecture.

No. 18 is a black laminated clay, 12 feet in thickness, full of the
impressions of Rheetic shells. The Avicula contorta is very abun-
dant, and attains double the size of our figured specimen. Awinus,
Cardium, Myacites, and other genera are also present.

No. 19, which rests immediately upon the above, is the equivalent
of the “Flinty Bed” of Beer-Crowcombe. Its lithological appearance
is precisely similar; but, although it contains many organic remains,
they are in so comminuted a state that very few are to be extracted
entire. On its outer surface are a few scales and teeth of Fishes of
the age of the Bone-bed, which, as at Beer-Crowcombe, is entirely
wanting, as a distinct bed, in this section, though it is to be found in
other places near Shepton-Mallet.

The blue clay, No. 20, I was unable to examine for organic remains.
The ‘‘ White Lias,” and the beds passing upwards, are not so well
represented as in other sections in the West of England, the beds
being thinner, more irregular, and without the clay-partings present
in the latter sections.

516 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [May 22,

EXPLANATION OF PLATES XV. & XVI.
PLATE XV.

. Sargodon tomicus, Quvensted¢, nat. size. Beer.
. Straparolus Suessii, Moore, natural size. Beer.
y 5 upper surface, enlarged.
RS " back view, enlarged.
by under surface, enlarged.
Gorvillia precursor, Quenstedt, right valve, showing lines of original colour,
eer
. Gervillia precursor, left valve. Beer.
ornata, Moore, enlarged. Beer.
. Lima precursor, Quenstedt, nat. size. Beer.
10. Avicula contorta, Portlock, nat. size. Beer.
TE ,; solitaria, Moore, enlarged. Beer.
12. Pleurophorus angulatus, Moore, enlarged. Beer.
13. ui left valve: worn. Beer.
elongatus, Moore, nat. size. Beer.
iy » ‘ight valve; nat. size. Beer.
16. Reda cloacinus, Quenstedt, enlarged. Beer.
depressus, Moore, nat. size. Beer.
elongatus, Moore, enlarged. Beer.
19. —— concentricus, Moore, left valve, enlarged. Beer.
ut KS right valve, enlarged. Beer.
21. 4 variety, enlarged. Beer.
22. ae Crowcombeia, Moore, lett valve, nat. size. Beer.
23. right valve, nat. size. Beer.
24, —— ”’ simplex, Moore, left valve, nat. size. Beer.
25. Leda Titei, Moore, perfect shell, slightly enlarged. Beer.
26. Modiola minima, Sowerby, nat. size. Beer.
27. » (?) young, enlarged. Beer.
28. Cardium Rheeticum, Merian, nat. size. Beer.

PLATE XVI.
Fig. 1. Myacites striato-granulata, Moore, showing the granulated surface, nat.
size. Beer.

2. Anatina? Suessi, Oppel, nat. size. Beer.
3. ? precursor, Quenstedt, nat. size. Beer.
4. Placunopsis alpina, Winkler, large valve, nat. size. Beer.
5. », exterior of small valve, nat. size. Beer.
6
7
8
9

Fig.

CIES | SOME LOT

i Peder Valoniensis, Defrance, nat. size.

. Arca Lycettii, Moore, nat. size. Beer.

. Myophoria postera, Quenst., right valve, enlarged. Beer.
5 es left valve.

10. 9 > left valve, showing denticulated carina.
11. Chemnitzia nitida, Moore, enlarged. Beer.
12. Henrici, Martin, enlarged. Beer.

13. Cerithium constrictum, Moore, enlarged. Beer.
decoratum, Moore, enlarged. Beer.

15. cylindricum, Moore, enlarged. Beer.
Rheticum, Moore, enlarged. Beer.

17. Natica Oppelii, Moore, enlarged. Beer.

18. Cylindrites fusiformis, Moore, enlarged. Beer.
ovalis, Moore, enlarged. Beer.

20. —— elongatus, Moore, enlarged. Beer.
oviformis, Moore, enlarged. Beer.

22. Trochus nudus, Moore, enlarged. Beer.
Waltoni, Moore, enlarged. Beer.

24. Ostrea fimbriata, Moore, nat. size. Vallis.
interstriata, Hmmerich, nat. size. Vallis.
26. Bivalve, uncertain, nat. size. Beer.

aT. nat. size. Beer.
28. Chiton Rheeticus, Moore, single plate, enlarged. Vallis.
29. interior, enlarged. Vallis.

30. Pollicipes Rheticus, Moore, enlarged. Vallis.

Quart. JourmGeoal. Soc Vol XVIT PI XV

Geo. West lith. W. West mip

RAATIG FOSSILS.

Mol XVI PL XVI.

a
)

Geol. 5o

Quart. Journ

Biinierd

eodvove

ei

lt

W.West, mp

Seo. West ith.

*

FOSSILS.

RH ATIC

1861. } SALMON—BOULDERS IN LODES. 517

June 5, 1861.

Joseph Tolson White, Esq., Mining Engineer, Wakefield, York-
shire, and William Boyd Dawkins, Ksq., B.A., Jesus College, Oxford,
were elected Fellows.

The following communications were read :—

1. On the Occurrence of Large Granite BovtpeERs, at a Great Depth,
in West Ros—EwaRNE Miner, Gwinrar, Cornwatt.
By H. C. Satmon, Esq., F.G.S.

At West Rosewarne Mine, in the parish of Gwinear, Cornwall, some
remarkable granite-boulders have been met with in the 50-fathom
level below the adit; the adit being 24 fathoms deep from surface,
this 50-fathom level is consequently 74 fathoms from surface.

The sections given in the accompanying figs. 1, 2, 3, show the
form and position of these boulders in the level. Their full size
cannot be ascertained, for they extend, as will he seen, into the roof
and south side of the level; but, taking those parts which are exposed,
there appear to be two large boulders, about 4 inches apart, the
eastern one projecting down 3 feet into the level, and the western
one projecting down 2 feet, as shown in the vertical section, fig. 2.
The length and width of these in the back of the level are shown
in the section (horizontal), fig. 3. The length of the eastern boulder
is 4 feet 2 inches, and that of the western boulder 3 feet 10 inches:
the width which they extend across the back of the level, from the
south side, is the same for both, viz. 2 feet 9 inches. The particular
form of these boulders, and their relative position to each other, are
fully shown in the sections; the vertical transverse section in fig. 1.
across the great eastern boulder, shows the manner in which it, and
a smaller granite mass beneath it, originally penetrated across the
level—the dotted lines marking the portions removed in excavating
the level.

Besides these two large boulders, there are also five other smaller
granite boulders or pebbles found in their neighbourhood. The di-
mensions of the sections of these latter which appear in the south side
of the level are—(1.) 14 inches by 53 inches; (2.) 22 inches by
12 inches ; (8.) 11 inches by 8 inches; (4.) 4 inches diameter ; (5.)
7 inches by 3 inches; all shown in fig. 2, in the order given, from west
toeast. It is worthy of remark that the two first-named—one lying
2 inches under the great eastern boulder, and the other lying a little
to the west of this, just under the point of contact of the two large
boulders—are more angular in form than either of the two large
boulders themselves, or either of the three remaining smaller ones.
Although the full size of the large boulders cannot be ascertained,
their probable size, judging from the portions exposed, would appear
to be nearly the same; that is, about 6 feet in width and depth,
with a length of from 4 feet to 43 feet.

The locality where these boulders are found is shown by the draw-
ing* No. II. The West Rosewarne Mine is supposed to be worked

* Not engraved with this paper.

518 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

Fig. 1.— Vertical Section across the Level at the line AB in fig. 2, show-
ing the original projection of the Boulders across the Level or Gallery.

a, a. Killas. 6, 6. Granite-boulders. c, c. Lode.

Fig. 2.— Vertical Section along the side of the Level, showing the
Granite-boulders on the South.

N41.

i WM RAMA
a, @. Killas. 6, 6. Granite-boulders.

Fig. 3.—Horizontal Section, or Ground-plan, showing the Boulders
in the Back of the Level.

YY
4

YY)
Y, MWY Y YY 4)
Hy Y YOY YY) Wh YY Y Vy /
a. Killas. 6, 2. Granite-boulders. c, c. Lode.

YY

1861. } SALMON-——BOULDERS IN LODES. 519

on the same lode as that wrought on in the Rosewarne United Mines
lying to the east, on the other side of the road. The direction of
this lode, which is about due east and west, extends east towards
the main granite-range of Crowan, which is about two miles distant
from West Rosewarne. In this mine, the direction of this main
lode is thrown out of its ordinary direction by taking a bend to the
left. At the point where (going west) this bend commences, a
branch-lode goes off with the same direction as the normal bearing
of the main lode: this lode is called the ‘‘ north branch ;” and it is
on the south side of this, lying in the “ killas” or “country,” that
the boulders are found. The sections given in figs. 1 and 3 accu-
rately show the position of the boulders with regard to this branch-
lode, which is here from 10 to 12 inches wide, the latter width being
the maximum of the lode as far as it has been seen in the ground
opened. Both the large boulders abut up close against the lode, but
do not extend into it.

I have said that the boulders are in the “ country ” or “ killas,”
which is so far correct that a defined line can be drawn between the
lode and the strata in which the boulders are imbedded. But al-
though this line can be drawn, there is yet a very striking analogy
between the two. The lode is almost entirely made up of breccia
(principally angular fragments of killas); and the “ country” in
which the boulders occur is also itself of a brecciated and conglo-
meratic character, containing numerous small boulders and pebbles
of capel and porphyry (elvan): they range from 4 inch, or even less,
up to 12 inches in diameter, and are called by the miners “ bullies,”
the small ones being called “young bullies,” and the larger ones
“srown bullies.” As a general rule, these rounded pebbles and
boulders seem to be found in the “ country ”’ in the neighbourhood
of the lode, but not generally in the lode itself, nor in the “ country ”’
at any distance from the lode. In none of the cross-cuts entirely
away from the lode, in what miners would call “‘ clean-country,”’ are
any of these boulders to be seen. Thus the lodes themselves seem
to be essentially breccia, rarely containing round boulders or peb-
bles. The “country” in the immediate neighbourhood of the lode
is also brecciated, but in a minor degree to the lode itself, and is
eminently characterized by these rounded boulders and pebbles ;
while the “country” at a distance from the lodes is generally quite
free from either breccia or pebbles, which, as far as can be seen,
seem to die out gradually, and not to cease at any definite line.
These facts seem to me to prove satisfactorily that there is a decided
relation between the lodes and these breccia and boulder-character-
istics of the “country,” which it should be our object to investigate
much more thoroughly and carefully than has hitherto been done ;
for, although similar phenomena have been frequently observed in
other mines in the same district, they seem to have been rather
regarded as matters of curiosity than investigated as facts which might
help to elucidate the conditions under which the lodes originated.

At Relistian Mine, west of West Rosewarne, and probably on the
same run of lodes, and at Herland Mine, to the north-west, on

520 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

parallel lodes, the occurrence of boulders and pebbles has long been
noticed and recorded, particularly in the ‘ Transactions of the Royal
Geological Society of Cornwall,’ which contain several references to
them. In vol. iil., in a paper ‘“‘on the Granite of the western part
of Cornwall,’’ p. 238, the late Mr. Carne thus refers to the pebbles
at Relistian :—

“The pebbles of the Relistian Mine are well known: here, at a
depth of 100 fathoms below the surface (which is not higher than
the surrounding country), a mass of pebbles was discovered in the tin-
vein, about 12 ft. in length, and nearly the same in width and thick-
ness ; and scattered pebbles were found in the vein far beyond those
boundaries. The pebbles are slate,—the same as the slate of the
country, which appears to have some chlorite in its composition,—
and are cemented together by a chloritic substance. In the crevices
between the pebbles, and connected with the cementing substance,
are oxide of tin and yellow sulphuret of copper; the former always
crystallized; the latter, never.”

In vol. v. p. 36, Mr. William Jory Henwood thus describes simi-
lar phenomena in the same mine and in Herland :—

“‘ At Relistian the slate contains numerous spheroidal concretions ;
some of them are compact, others schistose slate, and others are en-
tirely of quartz. In Herland, about 110 fathoms deep, there are nu-
merous nodular masses of granite, which consist of a base of felspar
with some quartz and a little mica; they are fine-grained and decom-
posing. They vary in size; and whilst some are not larger than a
hazel-nut, others are two or three feet in diameter. Both at Relistian
and Herland they are entirely enveloped by the slate, and have no
apparent connexion with each other; neither have the masses of
granite in the latter any contact with the lodes, or with any of the
small strings of quartz traversing the slate.”

In Table 36 of the same vol. v., referring to the 155-fathom
level in Relistian, Mr. Henwood makes the following note :—

‘“‘On both sides of the lode. but particularly on the north, the slate
is very soft, and opens in small joints: in this, round masses of slate
are often firmly imbedded. They are surrounded on all sides by
slate; but this structure, which prevails in many parts of the rock,
is only visible on breaking it. .... I was shown one round stone
of elvan which was said to have been found at 135 fathoms deep.”

As far as I can ascertain, however, nothing as yet has been found
at such a depth, at all comparable, either in size or character, with
the boulders I have described. The largest referred to are stated as
from 2 to 3 feet in diameter, while those I have described must be
at least 6 feet in diameter. The mineral character also is decidedly
different ; for the granite of the pebbles and boulders hitherto found
seems to have been invariably of a porphyritic character, with ery-
stals of felspar and quartz crystallized out of a base (probably fel-
spathic), and with very little mica. Boulders of this class have also
been found in West Rosewarne, east of the cross-cut, in the fifty-
fathom level at the point marked 4, and in the seventy-fathom level
at the point marked c, in the drawing No. Il. Specimens of these

1861.] SALMON—BOULDERS IN LODES. 521

are on the table ; and an inspection of them will show their marked
porphyritic character. On the other hand, the composition of the
two large boulders, and of the two smaller and more angular fragments
beneath them, is such as is essentially characteristic of a large granite-
mass, there being an entire absence of any porphyritic characteristics,
and an abundant development of mica. Now, the smaller porphyry-
granite boulders are, most probably, true granite, and derived from
a large granite-mass; but another hypothesis, which should assume
for them a derivation from some of the numerous elvan-courses
which traverse this district, would not be absolutely inconsistent
with the evidence of origin afforded by their mineral character ;
for elvan-courses do at times (particularly at considerable depths)
take an approximate porphyry-granite structure, and show some
mica: in their case, consequently, it would not be absolutely neces-
sary to assume their introduction from the surface; they might
have been introduced at considerable depths, and become rounded in
the lodes or broken country adjoining them. But in the case of these
large boulders, such a solution is scarcely conceivable. Their di-
stinctive mineral character places it beyond doubt that theyare derived
from a large granite-mass; and the distance of the nearest granite
from the locality where they are found seems to preclude any hypo-
thesis except that which would assume their introduction to have
taken place, by a fissure, from the surface. I leave out of the
question the hypothesis that these boulders can be considered as
being contemporaneous with the original deposition of the strata; for
it appears to me that their evident correlation with the other boulders
and pebbles (which, although not necessarily, nor, indeed, usually
found in the lodes themselves, have yet been recognized by long expe-
rience as haying anundoubted, aithoughill-understood connexion with
them), taken in connexion with the brecciated and conglomeratic
nature of the country in which they are imbedded, renders any such
suggestion quite untenable. The whole bearing of the evidence shows
that the boulders must be taken as having been subsequently intro-
duced, and most probably by a fissure from the surface.

Still, a solution of this kind presents some peculiar theoretical dif-
ficulties. The only plausible hypothesis of the formation of metal-
liferous deposits such as those of Cornwall—the only one capable of
giving even an intelligible explanation of their phenomena—is that
which assumes them to be, like granite and some other crystal-
line rocks, of an essentially hypogene origin,—to have necessarily
originated at considerable depths, and become subsequently exposed
by the action of denudation. But if these boulders were introduced
from the surface, the lode must be of a date subsequent to the un-
covering of the neighbouring granite-range by the action of denuda-
tion, and be held to have become opened and filled comparatively
near the then surface, instead of being hypogenc—of having originated
at great depths.

In searching for an elucidation of the obscure and complicated
eauses under which metalliferous lodes have originated, nothing is
more important than to endeavour to ascertain what periods of time

522 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

had elapsed between their formation and that of the eruptive rocks
with which they are generally associated, and which they usually
penetrate. Merely to ascertain, as we have already done, that the
lodes are generally subsequent in age to these rocks, is of comparatively
little practical value; what we want to know is, were they immedi-
ately subsequent, almost contemporaneous ?—or did long intervals of
time elapse between the formation of the one and the other? Another
important consideration is, to ascertain at what depth beneath the
surface—under what amount of cover—did they originate. .
Anything that can throw light on these subjects is of the highest
geologicalimportance. It seems to me that these boulder-phenomena
of Gwinear may have that result; but at any rate they are of great
interest as affording evidence of the physical conditions attending the
formation of, at least a certain class of, metalliferous lodes.

2. On an Erxcr Steriarra from the Sourn Joaerns, Nova Scorra.
By J. W. Dawson, LL.D., F.G.S.

(Abridged.)

TE erect trees so frequent in this celebrated coast-section, though
often distinctly ribbed, rarely show the minute markings of the leaf-
scars in a sufficiently perfect state to enable them to be compared
with those of the flattened trunks seen in the shales and ironstones.
This, no doubt, arises in part from the circumstance that the bases of
the trunks of Sigillarie did not always retain their characteristic
markings, and in part from the unfavourable influence of an erect
position in coarse and often laminated sediment. The specimen, to
which this note relates, and which I obtained in 1859 from a sand-
stone in Group XLV. of my section of the South Joggins*, affords an
_ exception to the generally imperfect condition of these trunks suffi-
ciently remarkable to merit a short notice.

The specimen measures 3 feet in height, and is 103 inches in
diameter at the base, 9 inches in the middle, and 73 inches at the
top, where it was abruptly broken off. At the base it shows the
usual tendency to divide into four main roots; but these have been
nipped off or flattened by pressure, not having been filled with sedi-
ment. The trunk retains its form on one side, but on the other the
bark has been rent from top to bottom, and in part folded inward.
This seems to have been caused by the pressure of the surrounding
sediment, and has probably somewhat diminished the diameter of
the stem. The interior of the trunk is filled with grey sandstone,
similar to that of the enclosing bed. The outer bark, less than a
line in thickness, is in the state of bituminous coal; and an internal
cast with a thin coaly envelope represents the pith. This internal
cast extends through the greater part of the length, but has fallen to
one side. It is only half an inch in diameter. The coaly matter
remaining on its surface shows, when prepared with nitric acid,

* Quart. Journ. Geol. Soc. vol. x. p. 6.

1861.] DAWSON—SIGILLARIA FROM NOVA SCOTIA. 523

cellular structure; and traces of transverse Sternbergian markings
remain in parts of it, so that it must not be regarded as the woody
axis, which has disappeared, but merely as the pith-cylinder.

The leaf-scars and other surface-markings are preserved throughout
the specimen, but only in a few places in sufficient perfection to show
the more minute features of the former. At the upper part the ribs
are very prominent, and there are twenty-six in the whole circum-
ference, the breadth of each rib being about nine-tenths of an inch.
On the outer or cortical surface each rib is flattened, or even concave,
along the middle, and strongly rounded at the sides, descending into
deep intercostal furrows; the flat mesial portion being smooth, the
lateral portions marked with sharp vertical ridges, and in places with
very delicate longitudinal and transverse strie. The leaf-scars extend
across the smooth middle portion of the rib, and are distant from each
other one inch vertically. In form they resemble those of Sigillaria
transversalis, S. Defrancii, and S. Brochantii, Brongt., being trans-
versely lanceolate, emarginate above, with acute lateral edges. Those
best displayed show two vascular punctures, with a third mark or pro-
minence between and rather below them. On the so-called igneous
surface, or that of the inner bark, the ribs are slightly furrowed or
striated lengthwise ; and the leaf-scars are represented by two deep
punctures of the vascular scars.

In tracing the ribs downward, some of them wedge out and dis-
appear ; so that at the middle of the length of the trunk there may be
about 22; each with a breadth increased to one inch and four-tentks,
and flatter than those at the top, with the intercostal furrow shallower.
The leaf-scars are now widened transversely, and have lost their
minute markings on the cortical surface; while on the ligneous
surface the vascular punctures are twice as far apart as at the top.
About the middle the vertical distance of the scars diminishes some-
what suddenly to seven-tenths of an inch.

In the lower third of the stem the ribs are quite obliterated, and
the whole surface is wrinkled with coarse waving strie or small’
furrows, due apparently to the expansion of the outer bark. The
leaf-scars still remain in regular vertical rows; but these are reduced
to about twelve, and apparently at the base to as few as nine. The
vertical distance of the scars is still about 0-7 inch; but the transverse
distance between the centres of the rows is increased to 2-8 inches
or more. In form the leaf-scars are now transverse furrows, an inch
or more in length, and the vascular punctures are half an inch or more
apart in each scar.

Of the roots I could obtain no specimens; but the markings on
the bark at the base of the trunk are precisely similar to those on
many Stigmarian roots found attached to less perfectly preserved
stems, and a few stigmaroid areoles are perceptible on the lower sur-
face of the stump.

The woody axis has entirely disappeared, nor does any mineral
charcoal appear in the base of the cast. It has either been entirely
removed by decay, or has been washed out by the waves before the
hollow bark was filled up.

524 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

As this trunk appears to belong to a species not previously de-
scribed, and we have a better knowledge of its parts and mode of
growth than of those of most of the named species, I may propose
for it a specific appellation, and would call it Si gullaria Brown in
commemoration of the many interesting discoveries in relation to
these plants made by my friend Richard Brown, Esq., of Sydney,
Cape Breton.

_ The author adds to this notice some remarks on points relating to
Sigillarie in general, illustrated by the specimen above-described :—
1. The evidence of the exogenous growth of Stgillaria*. 2. The
decadence of the leaves from the lower part. of the trunk in the living
state, and their abundance (as Cyperites), detached, in the coal-mea-
sures: the shorter vertical distance of the scars on the lower part of
the trunk, showing that, when young, the leaves were much more
crowded than subsequently: the absence of transverse bands of de-
formed and crowded scars sometimes seen on Sigillarie +, probably
connected with periods of fructification, and possibly occurring on
the upper part of the trunk only. 3. The difficulty of comparing
the characters of erect with those of prostrate Sigillarie. 4. The
species of Sigillaria found at the Joggins may amount to about
twenty ; and with reference merely to the habit of growth, without
regard to the resemblances or differences in the leaf-scars, these may
be arranged in three groups. ‘The first will include the present
species with S. reniformis, S. alternans, S. organum, and another
(S. ovalis, mihi) with oral scars lke those of S. catenulata but an
inch apart vertically. These have broad and well-marked ribs,
attain to a large size, and often occur erect. Other species with
narrow and less distinct ribs and more or less crowded scars, as
S. elegans, S. Knorrii, S. scutellata, S. Saulli, &c., do not appear to
have attained to so great diameter, and are more rarely seen erect.
In some of these species the markings and leaf-scars seem to be more
perfectly preserved to the very base of the trunk than in the species
before mentioned. A third group consists of species like S. Defrancit,
S. Menardi, &c., which are destitute of ribs and have the scars
arranged spirally. Some of these were of considerable diameter, others
quite small; but they are rare, and I have not recognized them in
the erect position. 5. The bast-like tissue of the inner bark of
Sigillarie is abundant in some of the coal of the Joggins; whilst
the discigerous tissue ¢ is prevalent in the great Pictou coal-seam :
the author thinks that in the former case the decomposition of the
vegetable matter was probably subaérial, or like that of a forest-soil ;
whilst the conditions of the latter were those of peaty bogs.

A résumé of the observations previously published regar rding Sigil-
laria, by Brongniart, Corda, and others, is added in the “supplemental
note to this paper.

* Quart. Journ. Geol. Soc. vol. x. p. 32.

t Ibid. vol. xv. p. 640.
t Ibid. vol. xii. p. 631.

1861. ] DAWSON—TRIGONOCARPUM. 520

3. Note on a Carpourte from the Coat-Formartion of Cape Breton,
By Dr. J. W. Dawson, F.G.S.

Aut the best authorities on coal-plants are disposed to refer the
seeds or fruits known by the generic names Z’rigonocarpum and
Rhabdocarpus to phenogams, and probably to gymnosperms. In
this case they may have belonged to Conifere or Sigillarie, or to
both. That they belonged in great part to the latter is, I think,
rendered probable by their occurrence very abundantly in the middle
part of the coal-measures where Sigillariw abound, by their various
forms corresponding rather to the many species of Sigillarie than to
the few of Conifers, and by their abundant occurrence in the interior
of hollow stumps of Sigillarie and in the surrounding beds. Still
these fruits or seeds may have belonged to very different plants ;
and, as an example of the type of structure most frequently associated
with Sigillarie, I have prepared a short notice of a species of which
very well-preserved specimens exist in my collection, and to which
I have assigned the name of

Tricgonocarpum Hooxeri. Figs. 1-5, page 526.

Numerous specimens of this species occur in a thin calcareous
layer in the coal-measures near Port Hood, Cape Breton. They are
not compressed, and are fossilized by cale-spar and iron-pyrites.
Their form is ovate,—the length being 0:3 inch, and the breadth 0-2
inch. The external surface is rough and destitute of distinct mark-
ings. Internally they present the following structures :—1. An
outer coat (testa), which is thick, carbonaceous, and apparently of a
dense cellular structure. This corresponds to the outer supposed
* fleshy coat’ of Lindley and Hooker; but in this species I think
it must have: been firm and hard, like the outer coat of the seeds of
pines, which it much resembles in appearance and structure. 2. An
inner coat (teymen or embryo-sac), which is thin and marked on its
outer surface with interrupted ridges, almost precisely in the manner
of the corresponding coat in the seed of Pinus pinea, This coat is
often pyritical, and in some specimens it presents toward the smaller
end indications of three ridges. It corresponds, no doubt, to the
outer coat of the ordinary Trigonocarpa. 3. A nucleus occupying
the whole interior of the last-mentioned coat, and exhibiting at the
smaller end certain wrinkles and a projecting tubercle, marking the
position of the embryo and micropyle. When the seed is sliced
longitudinally, the nucleus is seen to present an outer thick layer of
cale-spar, stained by vegetable matter, and an inner mass which is
colourless. In the smaller end, toward the micropyle, the remains
of the embryo and its suspensor are seen replaced by iron-pyrites,
in the manner represented in fig. 3. In some specimens the outer
coat appears as if divided into two layers, and the nucleus has
shrunk inward from the inner coat, presenting two additional sur-
faces, which may represent original lines of structure, but are, per-
haps, results of decay. A very similar species, which occurs in vast
abundance in the interior of an erect Sigillaria at the Joggins, has the

VOL. XVII.—PART I, 2N

526 PROCEEDINGS OF THE GEOLOGICAL SOCIETY, [June 5,
Figs. 1 to 5.—Trigonocarpum Hookeri, Dawson, from the Coal-
measures of Cape Breton.

Fig. 1. Fig. 2. Fig. 3.

Fig. 1. Perfect specimen, natural size.

Fig. 2. Specimen deprived of its outer coating.

Fig. 3. Broken specimen magnified.

Fig. 4. Section magnified: a, the testa; 0, the tegmen; c, the nucleus; and d,
the embryo.

Fig. 5. Portion of the surface of the inner coat more highly magnified.

outer coating very dense and coaly, and with a transverse fibrous
structure. In some specimens it shows a projecting ridge on each side,
and longitudinal striz, which might entitle it to be placed in the genus
Rhabdocarpus ; but no coal-fossils are more deceptive than these car-
polites, which, when flattened or deprived of their outer coats, pre-
sent appearances very dissimilar from those of the perfect condition.

I am by no means certain that this note adds much to the know-
ledge already possessed of the structure of Trigonocarpum ; but it af-
fords an additional example, and this of a species similar to those
most frequently associated with remains of Sigillarie.

1861. ] WHITAKER—RECONSTRUCTED CHALK. 527

4. On a Reconsrructep Bep on the top of the Cuatx and underlying
the Wootwicr and Rrapine Beps. By Wittiam Warraxer, B.A.,
F.G.S8., of the Geological Survey of Great Britain.

Ty a memoir illustrating Sheet 18 of the Map of the Geological
Survey of Great Britain (p. 21), I have noticed the fact that “at
Maidenhatch Farm, between Bradfield and Pangbourn” (over six
miles west of Reading), “there is a chalk-pit showing above 20
feet of rubbly chalk, with scattered blocks of chalk and irregular
lines of flint, overlying ordinary chalk. A similar bed of apparently
reconstructed chalk may be seen in a pit to the south of Tilehurst”’
(over two miles a little south of west of Reading), ‘‘ where it is
capped by the bottom-bed of the Reading Beds, so that the recon-
struction must have taken place before the deposition of the latter
formation.”

I have since seen a like bed, a short distance below the point
where the Chalk is capped by the Tertiary beds, in a pit by Batten’s
Barn, a mile north of Burnham, near Maidenhead. There was here
“about 18 feet of reconstructed chalk, with scattered flints and
blocks of chalk, and a line of flints near the middle. There were
some pipes of the drift-clay with flints, so common in chalk-countries,
in the top of this bed*.’’ This section and the one near Tilehurst
are clearly at the very top of the Chalk; but the one at Maidenhatch
Farm is on the flank of a valley cut through that rock.

In the neighbourhood of the Bedwins (in Wiltshire), near Marl-
borough Forest (in Sheet 14 of the Map of the Geological Survey
of Great Britain), there may be seen in many places, close by the
junction of the Tertiary beds (of which there are outliers in that
part) and the Chalk, a bed which seems to be made of reconstructed
chalk, and consists of pale-bluish and almost white clay, very chalky,
and containing small pieces of chalk, overlain by a confused mass of
pieces of hardened (?silicified) and somewhat flaggy chalk. This
latter is locally known as “‘ roach” (=rock); the fragments com-
posing it are as hard and tough as most crystalline limestones, and I
saw nothing at all like them in the chalk of the neighbourhood.

In making some deep drains down the hill-slope on the south of
Stoke Farm, west of Great Bedwin, this bed was found just at the
junction of the Chalk and the Woolwich and Reading Beds. I was
too late, however, to see whether it passed under the latter.

Just by the brick-yard, about three-quarters of a mile to the east
of the same village, there is much of this “‘roach”’ and the accom-
panying chalky clay, here again close by the junction of the Tertiary
beds with the Chalk: “roach” also occurs in the fields around, just
below the spots where the former come on.

Now this common occurrence of a reconstructed bed close by the
junction of the two formations, and there only, naturally leads one
to infer that it stretches beneath the later of them, the Woolwich
and Reading Beds. That a bed of a like nature is elsewhere found

. * From the MS. of a memoir illustrating Sheet 7 of the Map of the Geolo~
gical Survey.
2Nn 2

528 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

beneath that formation has been before shown; and there ean there-
fore be no reason why such should not also be the case near Great
Bedwin.

It is clear (even from the section near Tilehurst alone) that, whilst
in most places the Woolwich and Reading Beds rest on an undisturbed
surface of the Chalk (as may be well seen at Castle Kiln, Reading,
at the kiln north-east of Theale*, and at Shaw Kaln, Newbury?), in
others the latter formation has not only been denuded (as we know
it to have been from other reasons), but also redeposited, in a some-
what confused state, before the deposition of the former.

Whether a like bed occurs anywhere beneath the Thanet Sand I
know not. It is possible that the deposition of the reconstructed
bed near Tilehurst, &c., may have gone on at the same time as that
of this formation further to the east; both agree in occurring between
the Chalk and the bottom-bed of the Woolwich and Reading Beds.

I should add that the reconstruction above-noted is not the same
as that, of a later date, by which a gravel-like mass of pieces of
chalk and flints (with here and there a flint-pebble) has been formed
at the lower parts of some of the larger chalk-valleys, at the junc-
tion of the Low-level Gravel and the Chalk; nor is it to be con-
founded with the rubbly or flaggy structure that the Chalk often has
near the surface, and which is caused, I take it, by atmospherie
action alone.

5S. On some of the Hicrer Crustacea from the Britis Coat-
MEASURES. By J. W. Satrer, F.G.S., of the Geological Survey
of Great Britain.

Ir is almost as satisfactory to clear up the history of a little-known
or doubtful fossil as to discover one perfectly new. In the present
case we have both pleasures combined ; for the new and very perfect
Macrurous Crustacean here for the first time given from the coal-
measures illustrates and explains some published fragments, the
real nature of which ought not to have been so long misunderstood.
In Prestwich’s great paper on the Coalbrook-dale Coal-field, read

in 1836, and published some time after, a dubious Crustacean cara-
pace, very imperfect in some respects, was introduced in the same
plate $§ with the Zimuli. It is said, in the Explanation of the Plates,
that “the only living form to which Dr. Milne-Edwards could refer
it is the Apus cancriformis of the rivers of Central and Southern
Europe.” It was called therefore Apus dubius. The figure is more
imperfect than it need to have been; for the internal cast of the cara-
pace only is figured, and Mr. Prestwich’s collection contains the other
half of the nodule, a gutta-percha cast from which shows the true
external surface; and from this our figure 6 is drawn, only the other

* See Geological Survey Memoir illustrating Sheet 13, pp. 38 & 39.

+ Ibid. Sheet 12. Now in the press.

+ Transact. Geol. Soc., 2nd ser. yol. y. p. 415.

$ Op. cit. pl. 41. fig. 9.

1861. | SALTER—CARBONIFEROUS CRUSTACEA. 529

way upwards. The serrated border and the interrupted central
ridge are very clearly shown in both specimens and figures,

Again, in a paper in the Society’s Journal* “ on some Crustaceous
Remains in Carboniferous Rocks,” there is a short notice of some
specimens (or, rather, good electrotype copper moulds of the speci-
mens) presented to the Society by W. Ick, Esq., F.G.8S. These were
from the white-ironstone-measures of Ridgeacre Colliery.

One of these specimens was certainly anything but an Eryon, to
which Dr. Ick at first thought of referring it; and better materials
have enabled Prof. Huxley to describe it as a Schizopod or Stomapod
Crustacean of singular form, under the name of Pygocephalus Cooperit.
The other was a fine carapace (fig. 7), evidently identical with Prest-
wich’s Apus dubius, and was referred to by myself in Morris’s ‘ Cata-
logue,’ 2nd edit. 1854, as the remains of a Macrurous Crustacean.
I had then only just established the identity of the two fragments.
A more complete figure was afterwards given in Lyell’s ‘ Manual of
Elem. Geology,’ 5th edit. 1855, p. 388, under the temporary name
Glyphea, to which genus, however, it is not very nearly allied.

And now we have the entire form of a kindred species. This
most precious fragment (fig. 1) was brought to my notice by Dr. Ran-
kine, of Glasgow. It is in the cabinet of W. Grossart, Esq., of Sals-
burgh, by Holytown, who has liberally sent the rarity to London for
examination ; and I learn from Dr. Rankine that its place is in the
true coal-measures, above the uppermost limestones, and 960 feet
below the “ Ell-coal”’—in the band of ironstone termed the “ slaty
black-band.”

I will give the characters of this more perfect species first; and,
as the genus is not to be confounded with any of the Liassic or Oolitic
ones published by Von Meyer, Miinster, &c., I shall propose the
name Anthrapalemont for it. It is broader than the general form
of the Astacide, or than Glyphaa and its Liassic allies, but much
narrower than Eryon.

ANTHRAPALEMON, gen. noy.

Carapace scarcely so broad as long (except when crushed flat),
simple, flatter than semicylindrical, the sides a little arched out-
wards. Astrong central ridge in front, projecting as a thick (serrate ?)
spine, is separated by a concave space, or slight furrow, from a posterior
central ridge which only occupies (in the type-species, A. G'rossart?)
a small portion of the length. Front margin serrate. The outer
antenne have wide, square basal joints, apparently without any
advantage; the 2nd and 3rd joints not much oblique ; the rest about
as broad as long. Abdomen as broad as long, of six joints (besides
the telson), broad and very short ; the pleure, except the 2nd, pointed.
Telson very broad; appendages to the penultimate joint double on
each side, subtrigonal, broad.

* Vol. i. p. 199, 1844.

t Quart. Journ. Geol. Soe. vol. xiii. p. 336, pl. 13.

{ From dyv@paé, coal, and palemon, a prawn. The name has only a general
signification, and is not intended to indicate a real relation to Palemon,

530 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

Subgenus Paleocarabus. Type—Anthrapalemon dubius, Prestw.

Carapace rectangular-oblong, serrate in front and along the sides,
with a faint cervical furrow at the anterior third. Rostrum strong,
projecting ; posterior ridge prominent, complete to the hinder margin,
separated abruptly from the rostrum by the transverse furrow.

I have purposely restricted the characters of <Anthrapalemon
proper, because I think that the A. dubius may very probably turn
out to be a distinct generic form.

1. ANTHRAPALEMON GROSSARTI, Spec. nov. Figs. 1-4.

A. biuncialis, cephalothorace quadrato simplici neque tuberculis nec spinis late-
ralibus ornato; rostro valido serrato, } unciz et ultra 4 margine projecto ;
suleo cervicali obscuro; carina postica brevissima imcompleta; abdomine
(telsone lato trigono incluso) cephalothorace breviore.

Length, including the rostrum, 2 inches 1 line. Length of the
squarish carapace, without the rostrum (which projects 5 lines in
front), full 2 of an inch. Width of the carapace, when crushed,
exactly 1 inch; it was certainly not wider than long. It is only
serrate near the front; and at the anterior angles a strong spine
occurs. Body-rings 6 besides the telson, very short and very broad,—
the length of the 6 rings being barely equal to the breadth of the
abdomen, and even much less in the crushed fossil. The front ring,
as usual, with abbreviated pleurze; the second broadest (as in the
Lobster) ; the 3rd, 4th, and 5th narrower and pointed; the fulerum
not very conspicuous ; the articular area well marked out by a trans-
verse ridge.

Telson almost an equilateral triangle, broader above than its
length (the point is broken off, but was probably obtuse), Caudal
appendages two on each side, with thickened outer margins, trigonal ;
the shape, however, is not complete: when spread out, as in the
fossil, they extend beyond the width of the abdomen.

The entire surface of the carapace and body-rings is covered by
minute depressions, like those on the posterior half of the Lobster’s
carapace. The serrations on the rostrum are minute ; those towards
the anterior angles of the carapace are also minute, except the large
spines at the anterior angles.

Locality. Goodhock Hill, parish of Shotts, Lanarkshire: from the
“slaty band” of the black-band-ironstone, associated with Lingula,
Conularia, and Fish. Collection of W. Grossart, Esq.

2. AnrHRAPALEZMON. Op., fig. 5.

Fig. 5 represents in outline a pencil-sketch supplied to me by
Professor M‘Coy, seven years back, when I first mentioned to him of
the existence of this true Macrurous shield in the coal-measures.
He told me then that he had no intention of publishing his sketches.
T am not sure from what particular bed his fossil came, and shall be
glad of information : it was from the Glasgow coal-field. From the
rough sketch, it must belong to a much more elongate species than
A. Grossarti (“5 inches long,” according to M‘Coy in his letter),

1861. ] SALTER—CARBONIFEROUS CRUSTACEA, 531

Figs. 1—8. Macrurous Crustaceans from the Coal-measures and
Carboniferous Limestone.

eect
ee: ee eisai

1. Anthrapalemon Grossarti, sp.n. Nat. size. Lanarkshire. 2. Portion of the
Carapace enlarged. 3. Part of a Body-segment enlarged. 4. Some of the
Caudal Flaps enlarged. 5. Outline (from Prof. M‘Coy’s sketch) of a larger
species of Anthrapalemon. Lanarkshire. 6. Anthrapalemon (Paleocarabus)
dubius, Prestwich, sp. Nat. size. From Coalbrook-dale. 7 a. Another spe-
cimen, from Ridgeacre Colliery. 7. Portion of the Carapace enlarged.

8. a, 6, ¢. Palzocrangon? socialis, Salter. From Fife.

532 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 5,

probably even of a different genus ; but in the absence of specimens
it may be provisionally referred to Anthrapalemon rather than to
the next subgenus. The carapace in Prof. M‘Coy’s figure is smooth.

3. ANTHRAPALEZMON (Paleocarabus) pusrus, Prestwich, sp.
Figs. 6 & 7.

Apus dubius, Prestwich (from Milne-Edwards’s note) in Geol. Trans. 2nd ser.
vol. y. pl. 41. fig. 9, 1840. Macrura, remains of, Salter in Morris’s ‘ Cata-
logue,’ 2nd edit. 1854. Glyphea? dubia, Salter in Lyell’s ‘Manual,‘ 5th
edit. p. 388, 185.

A. (P.) biuncialis et ultra; cephalothorace oblongo-quadrato, tuberculis mino-
ribus spinisque marginalibus ornato ; rostro valido (serrato ?) a carina postica
longa completa omnino sejuncto ; sulco cervicali conspicuo.

Length of carapace, without the mucro, 13 lines; width 12 lines.
General form of the carapace (the only part known) rectangular-
oblong, the sides somewhat arched outward; the front truncate, the
hinder margin concave. ‘The rostrum, projecting nearly 3 an inch
in front, is strong and prominent at its base, but runs a very short
distance backward, and is then abruptly terminated by a wide con-
cave space, } of an inch broad, across which the cervical furrow,
margined by large spinous tubercles, is faintly indicated.

The posterior keel commences abruptly, and is continued as an
equal and rather strong ridge to the hinder margin; it is 3 an inch
long. The area on which it stands is flanked by two subparallel
furrows (indicating, | suppose, the cardiac region); and the whole
surface of the shield is rugose, as compared with that of A. Grossartt.
Scattered spinous tubercles occur also over all the elevated portions.
They are found, but of much smaller size, along the hollow space on
each side, and are absent on the broad margin. They are largest
around the rostral portion, two of them becoming spines in front.
The serrations on the margin are strong and equal, about 14 on each
side,—that at the outer angle not being stronger than the rest. The
characters of the surface, therefore, distinguish the section from the
type of the genus; and the two groups will, in all probability, be
hereafter regarded as distinct.

To complete the account of the Macruran remains occurring in
Upper Paleozoic rocks, it is necessary to refer to one or two other
fragments. One which Professor M‘Coy formerly thought to belong
to the Crustacea, and figured under the name Astacus Phillipsu
(Synopsis Carb. Foss. Ireland, pl. 23. fig. 1), was a very imperfect
fragment, and has been since recognized by himself and others as
merely an imitative portion of a brachiopod shell.

I am persuaded that I have seen a well-marked portion of a cara-
pace in the true Mountain-limestone of Derbyshire. It was col-
lected (among other treasures) by W. Hopkins, Esq., and still
exists, I hope, in the Woodwardian Museum, though its small size
may have caused it to be overlooked.

But if these be doubtful forms, there is one (fig. 8) which, now
that the existence of true Macrura, with the ordinary number of
segments, is known in the coal, can scarcely, I think, be referred to

1861. } SALTER—CARBONIFEROUS CRUSTACEA. Dod

the Amphipoda: I refer to the Uronectes (Gampsonyx) socialis,
mihi, published by the Rev. T. Brown in the Trans. Roy. Soc. Edin-
burgh, vol. xxi. p. 394.

The Uronectes (or Gampsony) of the Saarbruck coal-field (Paleeon-
tographica, vol. iv. p. 7, pl. 1) is described by Von Meyer as an
Amphipod with characters of the Decapods, especially of the Macrura
(‘eine Amphipode mit Charakteren der Decapoden, insbesondere de
Macrouren”’). It has 14 free segments. But the species from the
Scottish Carboniferous limestone (U. socials), figured by me for Mr.
Brown’s paper, has much fewer (only 6 or 7) definite body-rings, like
those of a Shrimp, with telson and caudal flaps, and, though indi-
stinctly seen, probably a long carapace. It was an error hastily to
compare it with Uronectes, and I will not commit another (until I see
better specimens) by attempting fully to settle its position. Mean-
time, as I have since seen other specimens, I think it will be desirable
to substitute the name Paleocrangon.

PALZOCRANGON, gen. nov.

Decapoda Macrura (Palemonide?). Asmall Shrimp-like crustacean, with short,
pointed carapace, and 6 or 7 body-rings, the front ones with expanded pleuree.
Telson small. Caudal appendages narrow, obovate. Feet —? Antenna —?

1. P. socialis, Salter, Trans. R. 8. Edin. xxii. p. 394. _ Carboniferous Limestone ;
Fifeshire. Fig. 8.
2. P.sp. Millstone-grit; Yorkshire, 1861. Undescribed.

These, it will be observed, are from the true Mountain-limestone
series and Millstone-grit below the Coal.

No Decapod has been yet observed in the Lower Shales of the Car-
boniferous formation, where large Phyllopoda (and Limulus ?) occur.

The Upper Devonian genus Gitocrangon, of Richter, figured
by that author in his ‘ Beitrige Palaont. Thuringerwaldes,’ pl. 2,
seems quite undeterminable. It is, I should think, even doubtful,
judging by the figures, if it be a Crustacean at all; but the descrip-
tion is by no means obscure, and the carapace, 7-ringed body, and
tail-flaps could hardly have been mistaken by so good an observer.

June 19, 1861.

John Atkinson, Esq., Memb. Phil. Geol. Soc. Manchester, Thelwall
near Warrington ; Major Nathaniel Vicary, Westgate, Wexford; and
Lord Rollo, 13 Upper Hyde Park Gardens, were elected Fellows.

The President made a commminication on the part of the Council,
that it is proposed to recommend to a General Meeting of the
Fellows in November that the payments of future Resident and
Non-resident Fellows be equalized.

It was proposed, seconded, and carried unanimously, that the
Best Thanks of the Society be offered to the President for the labour

534 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

and attention bestowed by him on the arrangement of the Foreign
Collections in the Society’s Museum.

The following communications were read :—

1. On the Linus of Denrrst Water around the Britisu IstEs.
By the Rey. R. Evrrzst, F.G.8.

[ Abstract. |
(The publication of this Paper is deferred.)

By drawing on a chart a line traversing the deepest soundings
along the English Channel and the Eastern Coast of England and
Scotland, continuing it along the 100-fathom-line on the Atlantic
side of Scotland and Ireland, and connecting with it the line of
deepest soundings along St. George’s Channel, an unequal-sided
hexagonal figure is described around the British Isles, and a pen-
tagonal figure around Ireland. A hexagonal polygon may be similarly
defined around the Isle of Arran. These lines were described in
detail by the author, who pointed out that they limited areas similar
to the polygonal form that stony or earthy bodies take in shrinking,
either in the process of cooling or in drying. The relations of the
100-fathom-line to the promontories, the inlets, and general contour
of the coast were dwelt upon; and the bearings that certain lines
drawn across the British Isles from the projecting angles of the
polygon appear to have on the strike and other conditions of the
strata were described.

After some remarks on the probable effect that shrinkage of the
earth’s crust must have on the ejection of molten rock, the author
observed that, in his opinion, the action of shrinking is the only one
we know of that will afford any solution of the phenomena treated
of in this paper, namely—long lines of depression accompanied by
long lines of elevation, often, as in the case of the British Isles,
Spain and Portugal, and elsewhere, belonging to parts of huge poly-
gons broken up into small ones, as if the surface of the earth had
once formed part of a basaltic causeway.

2. On the Orv Rep Sanpsrone Rocks of ForrarsHiRe.
By James Powrie, Esq., F.G.S.

Tue stratified rocks of Forfarshire, to the south of the Grampian
range, belong entirely to the Old Red Sandstone division of the
geological series. They consist chiefly of coarse grits, dark-red and
grey sandstones and flagstones, immense masses of conglomerate,
with intercalated flagstones, sandstones, and shales, marly and argil-
laceous shales, and some crystalline limestones or cornstones.
These, although in many instances broken up, and often faulted and
contorted by trappean outbursts, all rest conformably the one upon
the other. Thrown up against the flanks of the Grampian range at

1861. | POWRIE—OLD RED OF FORFAR. 535

very high angles, and dipping towards the south-east, some very
fine sections are afforded by the streams which, issuing from these
mountains, cut through the sandstones, in many instances in a line
almost at right angles to their strike. Of these the North Esk, the
West Water, the Noran, and the Isla may be mentioned as afford-
ing peculiar facilities for studying these formations. In all places
I have yet examined the Forfarshire sandstones are cut off from the
schists and slaty beds of the Grampians by considerable outbursts of
trap; it is, however, pretty evident that the sandstones overlie
these schists unconformably. Although I do not intend at present
to go at all into the geology of the Highland districts of Forfarshire,
I may here state that it seems to me highly probable that these
schistcse beds may be the equivalents of some portion of the Lower
Silurians. They apparently, for the most part, dip under the moun-
tains in a north-easterly direction ; but as this has in all probability
been occasioned by these beds having not only been raised up, but
actually tilted over, their true dip would seem to me to lie towards
the south-west, while the overlying sandstones dip towards the
south-east. In no instance have any organic remains been yet
found in any of these more northern beds.

The geology of the Lowlands of Forfarshire is upon the whole
exceedingly simple. It will be observed from the annexed section
that a synclinal line occurs at no very great distance from the
Grampians. This traverses the county in a line nearly parallel to
these mountains. The section also shows an anticline existing
about half-way between the syncline and the sea. This also runs
nearly parallel to the Grampian range: entering Forfarshire from
the German Ocean near to Montrose, it proceeds in an almost
straight line through Rossie Moor, passes along near to the villages
of Finhaven and Letham, crosses the south-east flank of the
Sidlaws; thence it continues onwards a little to the south of Tealing
and Baldovan House; west of Dundee Law, however, it bends off
towards the north-west, and passes in that direction into Perthshire.
Keeping these lines always in view, and also recollecting that
several great faults occur immediately to the north of the anticline,
all difficulties in the geology of the Forfarshire sandstones are readily
surmounted.

It may be observed that the section here given is little else than
a copy of that in Sir Charles Lyell’s ‘Manual of Geology*;’ they
only differ, I may say, in one particular, Sir Charles’s section show-
ing an overlying unconformable red sandstone, as found at Whiteness
near Arbroath. On examining the rocks at this place, this is found
to be undoubtedly the case. However, this overlying formation is
not found on that part of the coast where my section terminates‘.
At Whiteness the rocks consist of a coarse red sandstone with many

* 4th edit. p. 48 ; and see also Sir R. Murchison’s ‘Siluria,’ 2nd edit. p. 276.

+ This paragraph has been re-written since the paper was read, and the opinion
then stated (and published in the abstract of the paper), to the effect that the
unconformity shown at Whiteness in Sir C. Lyell’s section did not really exist,
is now abandoned by the author.—Ep.

[June 19,

PROCEEDINGS OF THE GEOLOGICAL SOCIETY,

536

Section of the Old Red Sandstone Formation in Forfarshire, from the Grampians to the Firth of Tay. Distance about 22 miles.

| <
m = :
Hi a
a f = g
Bie g 4
Ae 5 >: B= x
a a - 2 Se 2
at 5 1
2 pa | °
[= =| Coy ia} o So
a 3 oo 5 3
5: o e > i= S a
H I ; t
H H : H
: p H H
! :
3
ks ! '
a | G
4) 4
wm

A. Syncline.

B.
a.

Anticline.

Trappean outbursts. waza, This part very much broken up, the lower rocks re-
peatedly upheaved. «we. Great outburst, extending almost continuously from
Broughty Ferry to Red Head, bringing the lower formations again to the surface.
These traps for the most part consist of hard solid greenstones, occasionally,
although but rarely, assuming the form of columnar basalt, as in the bed of the
Isla below Reeky Linn, also felspathic and claystone porphyries and amygdaloids,

Concretionary limestone. y’, Lower bed. y. Upper bed.

Schists and slaty beds dipping under the Grampians.

Lower flaggy beds (tilestones?) with ripple-markings, impressions of rain-drops,
&c., with dull-red sandstones and grits, their place along the Grampians often
usurped by indurated or trappean conglomerates.

Conglomerates with intercalated red and grey sandstones, grey flagstones (Arbroath
‘“ pavement ’’), and shales, fossiliferous. Conglomerates towards the south of
Forfarshire giving place to reddish sandstones.

Great conglomerate, but little developed south of B.

e. Thick-bedded red micaceous sandstones with Cephalaspid remains.

Dull-red thick-bedded sandstones, marls, and shales, with round greyish spots.

Red sandstones, red and yellowish marls, much mottled with round grey spots, sup-
posed here to represent @ and e.

SS

- Sault.

Ps
o
= J
I foe} .
= is) Z = rs .
I a = * i 3 g
es $ ty td a ma =
o o a
“fe is cre ist - = gf
5 S 2 a 3 & g
= ao i) 2 = oO N
fa & 70) tr e Ou (ds) ‘
: | | i f I {
\ } H : ; i ;
; era i ‘
! ' L ’ ' H
H H ' H y H \\
: ‘ ! i 1
- o 1 1 t
1 ‘ H
{ ? ,

Note.—At the time I wrote out the accompanying description of the Forfarshire
rocks, I classed the spotted sandstones and marls lying betwixt the great outburst of
trap (marked in the above section # w) and the sea as belonging to the upper portions
of the Forfarshire sandstones. ‘This I was induced to do, after very considerable hesi-
tation, on account of these sandstones, &c., being very full of round greyish spots,
similar in appearance to those found in the red sandstones of Clashbinnie and Fife,
which are full of the scales and bones of Holoptychius, and thus undoubtedly the
upper beds of these formations; but since sending off the paper, I have been able to
procure from a bed of shale exposed on the banks of the Elliot, a small stream about
4 miles east from the line of the above section, Parka decipiens, with abundance of
vegetable remains, quite similar to those found in the shales of the Turin Hill flag-
stones. ‘These have only as yet been found in one stratum of this shale, but there in
very great abundance, and from this I have also procured the head and a plate of, in so
far as I can judge, a new species of Hurypterus. From this it would appear that the
above-mentioned eruption had again upheaved the lower Forfarshire beds, and that the
round grey spots are not confined to the upper beds,

The thickness of these formations may be roughly estimated as being not much
under 3000 feet. Col. Imrie, in his section of these rocks as exposed in the bed of
the North Esk, assigns 875 feet for the lower grits, and 1200 feet for the conglomerate.
Between the syncline and the Grampians they generally dip at very high angles, the
strata being in some instances almost perpendicular ; betwixt the syncline and the sea,
on both sides of the anticline, the dip seldom exceeds an angle of 22°,

1861.] POWRIE—OLD RED OF FORFAR. 537

imbedded pebbles, &c., evidently forming part of the upper portion
of the great conglomerate of Forfarshire, and having a clearly defined
dip of from 25° to 30° almost due south-east; but here, and also
in a small bay a little to the north-east, there is an upper conglo-
merate overlying these sandstones in a nearly horizontal position.
This conglomerate seems to be formed entirely of disintegrated por-
tions of the lower rock, from which most of the finer particles have
been washed away; it consists of water-worn pebbles in a siliceous
matrix, with intercalated layers of coarse red and whitish sandstones,
having all through, and especially in some of these intercalated
layers, angular fragments of sandstones, occasionally of large size,
with imbedded pebbles quite similar to portions of the lower rock. In
the absence of fossils it may be quite impossible to fix the true age of
this formation. Can it form part of the upper beds of the Old Red ?
This want of conformity has been observed in the Old Red Sand-
stone of other districts, and might fully account for the absence of
any equivalents of the Caithness-shire fossiliferous beds. On the
other hand, I have never observed any want of conformity betwixt
the lower Forfarshire rocks and the upper Holoptychius beds, or
betwixt these and the white Carboniferous sandstones of Fife; the
junctions of these formations are, however, very obscure. My
section is so far ideal, as I have introduced all the principal forma-
tions of Forfarshire, assigning to each, so far as in my power, its
proper relative position ; however, in no section of the county that I
know are all these to be found. The great features are, however,
pretty correctly taken from a line leading from the Grampians north
of Fearn Church, at nearly right angles to the strike of these rocks,
on to St. Andrew’s Bay, a little to the east of the village of Car-
noustie.

Commencing with the lowermost of the Forfarshire formations,
we find a very considerable thickness of dark-red gritty beds, having
very close to their base an intercalated bed of concretionary lime-
stone or cornstone. Nowhere along the hills in Forfarshire is this
bed exhibited ; in Kincardineshire, however, it occupies a moderately
prominent position, having been wrought to some extent at the
Clattering Brig, at the south base of the Cairn o’ Mount in the
ravine a little to the east, called the Slack of the Birnie, and in
other places. This same limestone has also been wrought where
these formations have been again thrown up north of the anticline,
at Millton of Mathers, and near the Dubton Station of the Scottish
North-eastern Railway (both places in Kincardineshire), and at Bud-
donness, south of the anticline in Forfarshire. It is also found near
Newburgh in Fifeshire, occupying the same relative position. Some
distance above this limestone dark-red and rather indurated flag-
stones are also intercalated in these grits. These are well seen in
a quarry on the north-west side of the road leading from the Clat-
tering Brig towards Feltercairn, also in the bed of the West Water,
underlying the conglomerates of Catterthun Hill; they are again
thrown up and exposed at the fishing-village of Ferryden. Prof.
Harkness suggested to me (and I think with much probability), that

538 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

these might be the equivalents in time of, and here represent, the
tilestones of the English formations. These grits pass upwards into
conglomerates of very great thickness; in many localities their place
is entirely usurped by the conglomerate. When this is the case, the
conglomerate immediately succeeds the trappean outbursts, cutting
off the sandstones from the schists; and here the matrix in which
the pebbles are imbedded is almost always highly indurated, and
possesses an almost trappean aspect. This matrix as it rises softens
down until it becomes very similar in composition and hardness to
the sandstones overlying and intercalated with the upper portions
of this conglomerate. These conglomerates are thrown up in enor-
mous masses along the flanks of the Grampians, forming a lower
and interrupted range of hills, rising in several instances to heights
of over 1000 feet above the sea-level. At some considerable ele-
vation above the red-coloured flagstones or tilestones above men-
tioned, and near to where the indurated matrix softens down,
are found intercalated (or rather, from their persistence, interstra-
tified) flaggy beds, consisting of greyish thin-bedded and other sand-
stones, and greenish- and other coloured argillaceous shales. These,
although by no means largely nor persistently developed to the
north of the syncline, assume, when again elevated by the anticline,
an importance beyond all the other deposits of Forfarshire ; being
not only largely wrought for economic purposes, but affording the
only prolific fossiliferous beds of that county ; I will therefore again
revert to them. The upper portion of the conglomerate is very
persistent in character along the Grampians, extending in a direction
from nearly north-east to south-west almost from the German to
the Atlantic Ocean. When the conglomerate is upheaved, however,
by the anticlinal outbursts, this persistency ceases. To the north of
this the conglomerate is still found in very large masses, as in the
Garvock range of hills in Kincardineshire, and in the hills of Fin-
haven in Forfarshire. To the westward, as in the Sidlaw Hills,
the conglomerate very much thins out; its place being almost alto-
gether taken by sandstones, for the most part thickly bedded and
varying in colour from bluish grey to greyish red. Still further to
the west, however, we again find the same conglomerate very largely
developed in Perthshire, as in the Ochil range to the north of the
Bridge of Allan. Passing the anticline, the conglomerate is again
seen in the section afforded by the coast betwixt Montrose and
Arbroath, where it forms the bold promontory called the Red Head,
from whence it extends on to beyond the fishing-village of Auch-
mithie, All along this line the action of the waves has cut it out
into most picturesque gulles, ravines, and caverns. In the inland
parts of Forfarshire, to the south of the anticline, it is only found
intercalated, in not very considerable quantities, with the red and
grey sandstones, which here seem in great measure to have usurped
its place. In the upper portions of the conglomerate, intercalated
beds of coarse red sandstones become more and more abundant,
until at last this formation passes entirely into thick-bedded sand-
stones, generally highly micaceous, and affording an excellent and

1861. ] POWRIE—OLD RED OF FORFAR, 539

durable building-stone of a rather pleasing red colour. Nearly where
the conglomerate passes into this sandstone is found in some places
north of the anticline an intercalated bed of concretionary lime-
stone, very similar in character to the already-mentioned lower bed.
This has been wrought, although to no great extent, in several
places, as at Trinity Muir, near Brechin, Strickathrow Hill, and
in Kincardineshire in the Garvock range. A sandstone of a dull
deep-red colour, soft, and weathering fast on exposure to atmospheric
influences, is generally found overlying the above-mentioned mica-
ceous sandstone; this being again overlain by deep-red and also
sometimes by whitish and greyish marls and shales, forming the
uppermost of our Forfarshire Old Red Sandstones. These are re-
markable, and may be pretty readily distinguished by being very
full of peculiar greyish-coloured round spots, varying in size from
about one-tenth of an inch to over one inch in diameter. In many
instances these are so numerous as to give the sandstones quite a
mottled appearance. These overlying sandstones are, however, by
no means very persistent either in character or appearance; in some
instances one or other being absent, while in many cases they seem
to pass into one another.

Until comparatively a recent period the Forfarshire rocks were
considered as particularly destitute of fossils, and even yet the known
fossiliferous deposits are principally, if not altogether, confined to
the flagstones and shales intercalated in the conglomerate. In no
instance have any of the limestones as yet yielded any trace
of organic remains ; and equally destitute of these have all the upper
marls and shales as yet proved. In giving a very short notice of
such of those deposits as have shown any vestiges of the plants or
animals existing in times of such remote antiquity, it may be well to
take them in the order of their superposition. Lowermost we have
the dark-red, rather indurated flagstones; and even in these as
yet no recognizable remains, either animal or vegetable, have been
found. Their beautifully perfect ripple-markings, however, prove
that they had been deposited in a shallow sea over which the winds
blew and the waves rolled ; and being in some instances completely
covered with trails of Crustaceans and Annelides, the existence of such
cannot be doubted, while deeply pitted indentations, as of rain-drops,
show that the sands.nd muddy banks of these shores, when uncovered
by the tide, were not without rain. The Rev. Hugh Mitchell, whose
labours have added so much to our knowledge of the Forfarshire
organic remains*, has in his collection several beautifully character-
istic slabs of these flagstones, dug by him at Ferryden, where they
have been upheaved. Considerably above these and intercalated in
the conglomerates are found the beds already mentioned, from which
the well-known Arbroath “pavement” has been so largely dug. These
are highly interesting to the geologist, as affording samples of all the
organic remains that have yet been found in Forfarshire; indeed,
with the exception of Cephalaspis, which has been recovered from
sandstones considerably overlying them, none other of the Forfarshire

* See above, p. 145, &e.

o40 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

rocks have yet yielded any organism, whether animal or vegetable.
These beds consist of thin- bedded grey flagstones, red and grey
sandstones of some thickness, and greenish and bluish argillaceous
shales. In these by far the most abundant organism is the Parca deci-
piens ; next plentiful are the remains, commonly broken, of segments
of the great Forfarshire crustacean, the Pterygotus Anglicus. These as
well as the Parca are found more or less well preserved in both
shales and sandstones ; with these are associated the remains of other
Crustacea, as the Stylonuwrus of Mr. D. Page. Annelid-tracks and
burrows are also occasionally to be met with in the sandstones. After
these, but much more rare, are found portions of the head-plate of
Cephalaspis ; anything approaching to complete specimens of this
fish being very seldom found in any of the many localities where

these flagstones are largely wrought. A peculiar ity regarding the
remains of Cephalaspis is, that they are always found in the sand-
stones; I have never yet seen the smallest vestige of them in any
of the shales, although full of other remains: occasionally a fish-
spine may also be picked up. The Farnell Beds, which have yielded
so many interesting vestiges of the very remote period when these
flagstones and shales were deposited, belong to this same portion of
the Forfarshire sandstones. They were noticed several years ago by
the Rey. Mr. Brewster, of Farnell, as likely to prove fossiliferous.
It is to the Rey. Mr. Mitchell, of Craig, that we are indebted for first
discovering the nature of these fossils ; his indefatigable researches
were rewarded by the discovery of two small Ganoid fishes, named
by Sir Philip Egerton Acanthodes Mitchel and Climatius seutiger ;
also several varieties of Crustacea. The liberality of the Earl of
Southesk has since largely opened up this deposit, and allowed its
treasures to be examined and preserved to a great extent by Mr.

Brewster and myself. My only regret is that, from the dip of strata
making the working now not only expensive but difficult, and no
product of economic value being obtained from it, it must be looked
on as all but exhausted. We have, however, already been able to
add to the above-named fishes several others, mostly as yet unnamed ;
amongst these is a Diplocanthus, named by Sir Philip Egerton D.
gracilis ; also a goodly sized Placoid, at present being described by this
distinguished ichthyologist. Several remains of Pteryqoti and other
Crustacea have also been found; some of them apparently new. Mr.
Walter McNicol at Tealing has since discovered several localities,
mostly in the Sidlaws, where the same fishes are to be found, although
not so perfectly preserved. It is worthy of remark that the common
colour of the shales, which alone are fitted for preserving such or-
ganisms, belonging to these flagstones, is of a light greenish hue ; in
these no vestige of ichthyic remains has yet been found. The colour
of the shales where Mr. McNicol has found these fishes, &c., is hight
blue; while the Farnell shales vary from a fine cream-colour to a
dark grey. The vegetable remains of these beds are generally very
imperfect and unreadable. ‘The only instance in which a plant
clearly belonging to the land has been disinterred occurred about
twenty years ago, when what was called by the quarrymen a small

1861. ] POWRIE—OLD RED OF FORFAR, 541

tree was dug out, and by them cast aside as useless. On hearing of
this discovery, unfortunately not until months elapsed, I could recover
only a small portion of the root, seemingly of some Lepidodendroid.
This was noticed and described, from data furnished by me, by the
late Hugh Miller at the Meeting of the British Association held at
Glasgow in Sept. 1855 (see his ‘ Testimony of the Rocks,’ p. 447).
Generally these vegetable remains appear to have formed parts of
marine or at least aquatic plants. None of the other sandstones inter-
calatedin the conglomerate have yet proved fossiliferous. ‘The mica-
ceous solid-bedded sandstone, however, into which it has been stated
the conglomerate passes, has yielded some of our finest specimens of
Cephalaspis (no crustacean remains are found in our rocks overlying
the flagstones). The rock near Bridge-of-Allan, whence I procured
the two specimens of Péeraspis now in Professor Huxley’s hands,
occupies identically the same position as this sandstone, and although
lighter coloured, its lithological character in other respects is quite
similar ; and although no specimens of this fish have yet been saved
from the rocks in Forfarshire (these specimens being the only ones
yet recognized in Scotland), yet I have little doubt that it is not
altogether wanting there. Indeed I suspect that some specimens from
this same sandstone, which, I must confess, I years ago cast aside as
mere worthless fragments of Cephalaspis, were in reality portions of
the head-plates of Pteraspis.

From none of the other and upper beds of Forfarshire have any
fossils of any kind ever yet been obtained; their quality rendering
them unfit for building, and generally being covered by the rich clays
of the Valley of Strathmore and its continuation, the opportunities for
studying their nature are not so frequent. Whether they are the
equivalents of the red Holoptychian beds of the Carse of Gowrie
(Clashbinnie, &c.) is yet to be determined. One thing is deserving
notice—namely, that they are, equally with the Carse of Gowrie, red
sandstones much mottled with circular spots of a greyish colour.
Although I have examined hundreds of these spots in the Forfarshire
sandstones, in‘no instance, however, have I detected anything organic
in them; while Dr. Anderson, of Newburgh, states* “that portions
of scales and minute bones have been detected in the centre of the
spots” from sandstones belonging to the Carse of Gowrie.

It is now allowed that the lowermost of our Forfarshire sandstones
belong to the lowest of the Old Red formations, thus underlying the
Caithness beds, &c.; their peculiar Crustacea as well as the Cephalaspid
remains evidently closely uniting them to the Upper Silurians ; while
at the same time the Ganoid fishes, belonging in some cases to the
same genera, and in other respects much resembling those of the
more northern rocks, indicate also a near alliance with these forma-
tions. Again, ourupper beds, if not identical with, evidently as nearly
approximate to, the Holoptychian sandstones of Clashbinnie, &e. No
want of conformity in our Forfarshire rocks shows any break in the
continuity of these deposits ; yet nowhere have I detected what could
be considered the equivalents of the Caithness beds. Does this in-

* «Dura Den,’ p. 26.
VOL, XVII,—PART I. 20

542 PROCEEDINGS OF THE GEOLOGICAL society. [June 19,

dicate the probability of an immensely lengthened period during
which there was gradual sinking, followed byas gradual an uprising of
the sea-bottom, unaccompanied by any of those violent volcanic
eruptions so common during the Carboniferous era? Several reasons,
in my opinion, concur in rendering this by no means improbable.
That these deposits were accumulated during a period of comparative
quiescence is shown by the entire absence of intercalated traps or
other igneous rocks. The Forfarshire sandstones are very fre-
quently found disrupted, they are often overlain by large flows of
igneous matter, intruded traps are found all over the county ; but in
no place have I ever yet seen these traps again overlain by the sand-
stones, thus evidently proving the trap-rocks to belong to a later
geological epoch. <A gradualsubmergence is, I think, equally clearly
indicated during the period while the lowermost rocks were being
laid down; the very undermost of our fossiliferous beds with their
beautifully preserved ripple-markings, Crustacean trails, and even
rain-prints, evidently point to a sea-beach left frequently dry by the
ebbing tides. Above these the shales, mixed up with the sandstones
full of Vegetable and Crustacean remains, still indicate ebb-waters ;
but now the ripple-markings, although yet to be seen, are much less
distinct, Crustacean or other tracks become exceedingly rare, and
rain-imprints cease to be recognized ; the Cephalaspis, a fish evidently
haying a wide range in time and space, is found, all showing a
sinking of the sea-bottom. Still rising in the series, we find that the
sea has further deepened; the conglomerates, only formed near a
shore, cease, and sandstones, having no organic remains except an
occasional Cephalaspis or Pteraspis, take their place ; still the sea
deepens and the land recedes until almost no deposit, and what there
is barren of organic remains, takes place. A long period intervenes
during which the Caithness beds form the bottom of shallower, or
at least much more life-sustaining waters. At last this depression
comes to a close, and as gradual an upward movement takes place ;
and again sediments are accumulated, now entombing a new class of
animals, the Holoptychius and his allies taking the place of Cepha-
laspis and the Crustacea of the more ancient ocean. This upheaval
continues, violent volcanic commotions take place, and Forfarshire
from being a sea-bottom becomes high land, while in the lower
districts the coal-measures are being accumulated.

8. On the Luptow Bone-Bep and rts CrustacEAN REMAINS.
By J. Hartey, M.B. Lond.
[Communicated by Prof. Huxzey, Sec. G.S., &e.]

{Prare XVII.]

Ir is well-known to geologists, that between those two great systems
of rocks the Silurian and Old Red Sandstone, there occurs an inter-
mediate series of relatively small development, which, as it partakes

1861.] | HARLHY—ASTACODERMA. 543

of the lithological and paleontological characters of both systems,
has been well called “ Transition-beds.”

Transition-beds with contained Bone-beds.—That part of these
beds which immediately overlies the Upper Ludlow Rock is com-
posed of soft argillaceous shales; and that which immediately under-
lies the Old Red, of a soft, yellow, fine-grained sandstone—the Down-
ton Sandstone.

Just below the Downton Sandstone, and therefore in the lowest
partof these transition-strata, appears that remarkable animal-deposit
called the “ Ludlow Bone-bed”’; and just above the Downton Sand-
stone, standing indeed within the threshold of the Old Red, another
animal-deposit occurs, rarely, however, as an isolated conglomeration
of organic remains as in the bone-bed, but most commonly haying
these more or less freely diffused throughout argillaceous and are-
naceous strata, or a gritty calcareous conglomerate which often be-
comes a compact bluish limestone. Thus, to speak generally, we have
a lower bone-bed more appertaining to the Silurian system than to
the Old Red; and an upper, more diffuse one, much more closely
associated with the Old Red than with the Silurian Rocks. Both
have their types at Ludlow,—the former in Ludford Lane and the
north-eastern slopes of Whitcliffe ; the latter in the strata exposed
on the south bank of the Teme, opposite to the Gas-works and Paper-
mill.

_ Ludlow Bone-bed.—Iit is to the older and lower, or Bone-bed
proper, that I would draw attention, premising a few general remarks.
The Ludlow Bone-bed was at first considered to be a local deposit ;
but later researches have shown that it extends interruptedly over
an area of forty or fifty miles*, a fact which renders probable that it
will be found to have a still more general distribution. As it occurs
at Ludlow and in its neighbourhood it forms a thin seam, varying in
thickness from half a foot to the eighth of an inch, or rather to
nothing ; for it gradually thins away, and here and there disappears
altogether, and we consequently fail to trace it for a distance. In-
terruptions which thus occur locally and on a small scale may pro-
bably occur on a large one throughout these early rocks, and so ac-
count for the absence of the bone-bed in wide geological areas.
Whenever it does occur, it becomes an infallible guide to the geologist.

Sir R. Murchison has described the bone-bed as being composed
of “a matted mass of bony fragments, some of which are of a
mahogany hue, but others of_so brilliant a black, that, when first
discovered, they conveyed the impression that the bed was a heap of
broken beetles” (‘ Siluria,’ second edit. p. 148). The bed is often
very compact and of a lighter colour, and closely resembles the cake
from which linseed-oil has been expressed.

All that we know of the constituents of this remarkable deposit is
contained in about two pages of the text and an illustrative plate of the
‘Silurian System.’ There we learn that, with the addition of afew
molluscan shells, it is composed of the remains of Sclerodus, Plec-

* *Siluria,’ and Quart. Journ. Geol. Soc. vol. ix. p. 11.

+ The remains of Molluscs occurring in this bone-bed belong to Discina

202

544 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

trodus, and Thelodus, which are stated to be fishes*. Length of
time has rendered us familiar with these names, but has failed, except
perhaps with regard to one of them, to extend our very imperfect
knowledge of the animals which they serve to designate. And this
is not to be wondered at; for the remains are so very fragmentary,
brittle, and coherent, that the utmost patience and no little labour
are required to enable one to succeed in obtaining any definite results.
Difficulties, however, do but enhance the interest which naturally
attaches itself to this deposit ; for, whenever and wherever animal
life may have been first endowed with forms which characterize that
highest type of it called vertebrate, it is in this bone-bed that we
find the first assurances of the varied existence of this type. I say
“‘varied;”’ for the Ludlow rocks have furnished a single species of
Pteraspis, which seems to haye appeared in almost solitary dignity
to proclaim the dawn of a higher existence to a world of Crustaceans
and Molluscs. To ascertain in what forms this higher existence,
as we find it in the bone-bed, begun—whether it was some creation
distinct from both that which preceded and that which succeeded it,
or whether it is one of the necessary connecting links in a progressive
development of life which runs uninterruptedly throughout the older
rocks, are the inducements to the careful study of this complex mass.
In examining this deposit, however, there are other and more pre-
liminary questions which require to be answered first; and it is the
solution of one of these which is the chief object of this paper.

Crustacean life in the Silurian age.—The Silurian was essentially
a Crustacean age, and one that maintained its full vigour throughout
the transition-strata to which I haye referred. My first endeavour,
therefore, was to ascertain whether the bone-bed contains Crustacean
remains. I find that it does, and in no inconsiderable quantity ; and
I now proceed to lay the evidences before you.

Crustacean remains in the Ludlow Bone-bed.—On making diligent
examination of the broken and washed deposit, with the aid of a
pocket-lens, I find a number of minute bodies of various but often
related forms, which, for convenience of general description, I will
divide into three classes.

1. Of the bodies which I have placed in the first class, some re-
semble the minute conical teeth of osseous fishes, others appear to be
made up of two, or occasionally of three such teeth (figs. 1-4).
Rarely, one meets with what at first sight appears to be a very
minute jaw set with a row of conical teeth (fig. 15), and more rarely
still, with microscopic curved fangs or spines (fig. 16).

rugosa, Lingula cornea, Orthis lunata, Rhynchonella navicula, and some indeter-
minable genera.

* T have submitted all the remains which are thus designated to careful micro-
scopical examination, and find that they possess a true bony or dentinal structure.
While I thus disprove Prof. McCoy’s supposition that Plectrodus and Sclerodus
are Crustacean fragments (Quart. Journ. Geol. Soc. vol. ix. p. 14), I agree with
him that the parts figured in the ‘Silurian System’ under these names cannot be
teeth or jaws; they are, I believe, the posterior spines of the cephalic plate of
some Cephalaspidean fish,

1861. ] HARLEY—ASTACODERMA. 545

These last two varieties are very interesting as being in external
form, and, as I will show, in all other respects, identical with Pan-
der’s ‘‘ Conodonts.”

In an elaborate monograph on the fossil fish of the Silurian system
of the northern part of Russia, Dr. Pander has described a host of
tooth-like bodies which he has assumed to be the teeth of Fishes,
and to which collectively he has given the term ‘“ Conodonts,” and
subdivided them into 13 genera, comprising 56 species. They are
of two kinds, simple and compound. The simple resemble minute
spines about a line in length; under a magnifying power many of
them look like the stout curved thorns of a rose-stem ; they are plane,
or furrowed longitudinally, more or less compressed and hollow at
the base, which is expanded with an everted margin. The com-
pound ones are larger, and resemble small jaws, each beset with a
row of conical teeth, which may be equal or unequal, the row being
often terminated and sometimes interrupted by larger fang-like ele-
vations. These Conodonts were at first stated to be composed of pure
carbonate of lime ; but on re-examination, they were found to con-
tain phosphate of lime also, which strengthened Dr. Pander in his
supposition that they were fish-remains. As described by him, they
are white and opake, with transparent edges,—or reddish-yellow,
transparent and horny looking, and under a high magnifying power
show nothing but homogeneous superimposed layers.

2. To return to my own forms. The second class of bodies may
be hkened to the crown of a bicuspid or molar tooth, and especially
as we should find them beneath the gums of a new-born child
(figs.5, 6,9). The upper surface presents three more or less elevated
and rounded cusps; the lower surface is excavated into depressions
corresponding to the cusps. This form, on the one hand, by losing
elevation, becomes a mere tuberculated plate or scale; and on the
other, by lateral extension of the ridges joining the cusps, the little
bodies present a V-shaped elevation (fig. 11). By the combination
of two such, we have an undulated plate surmounted by a W-shaped
elevation (fig. 12).

The bodies included in the first and second classes are very hard,
have a rich brownish-red or amber colour, and are semitransparent,
and highly polished. When possessed of but little colour, they
appear to be composed of discoloured ivory, and occasionally present
longitudinal converging strie, due to coloured lines traversing the
semitransparent substance ; sometimes it is difficult to say that these
are not linear elevations. __

From their external form and ivory-like consistence and appear-
ance, I was at first induced to think that some of these tooth-like
bodies were teeth, probably of Fishes; but the variations presented
by others, and their declination into mere tuberculated plates, ulti-
mately persuaded me that this could scarcely be a correct supposition.

3. In the third class we find small thick plates of a somewhat
oblong form, not exceeding two lines in length, and about a fourth of
a line in thickness. There are three pretty distinct varieties. The first
is distinguished by having one of its surfaces raised into three nearly

546 PROCEEDINGS OF THE GEOLOGICAL society. [June 19,

equal rounded tubercles, bounded (at least in one direction) by the
slightly elevated margin of the plate (fig. 18). The second is some-
what pyriform in outline, and presents usually one small tubercle
at the narrow end; sometimes there are two, and occasionally three,
more or less separate and distinct (figs. 19, 20). The third variety
occurs as oblong or rounded plates either plane or with one surface
slightly concave and the other slightly convex.

The bodies placed in this class are commonly of a greyish or
blackish-brown colour ; and a fractured edge presents an excessively
fine fibrous structure.

All the forms included in the above three classes, and all their
varieties, possess the same ultimate microscopical structure and che-
mical composition,

Structure.—The structure, which is perfectly preserved, is unmis-
takeably Crustacean. A microscopic section presents a vertical tubu-
lar, and a horizontal laminated structure. In the flattened bodies
these two structures are strictly perpendicular to each other; but
in the conical bodies, except about the apices, they have a more or less
oblique relation (figs, 12 b, 12).

The tubes are excessively fine, varying from about the=,4,, to
the s<}p;th of an inch in diameter. In most specimens they appear
to be injected with a reddish-brown material; but this rather stains
the walls of the tubes than fills up their cavities; for in transverse
section they appear as clear dots with a discoloured circumference,
and on placing the bodies in hot turpentine, minute air-bubbles are
freely displaced. The above is therefore probably an overstatement
of their real size. The tubes are so crowded, that there appears, in
vertical sections, to be little or no intertubular substance ; they lie
parallel to each other, and never branch; and when the surfaces
between which they pass are parallel, they take a straight course ;
but whenever an elevation occurs, the tubes, instead of converging
towards the apex, take a slight bend outwards to either side of it,
Minute, rounded or oval, calcareous corpuscles, measuring about the.
=ypyth of an inch in diameter, are often present. In horizontal sec-
tions, the tubes appear to be arranged in systems forming rounded
sinuosities separated from each other by clear tortuous lines of in-
tertubular substance (fig. 20 a).

The horizontal lamination presents the appearance of a great num-
ber of excessively fine, and usually faintly marked, wavy lines, the
undulations of which are very minute, regular, and parallel to each
other (fig. 12 d). The Conodonts possess the same structure. The form
called Gnathodus Mosquensis, tab. 2a, fig. 10 in Pander’s work, of
which I have found several specimens in the bone-bed (one is de-
lineated in fig. 15), shows both the laminated and tubular structure ;
the tubes, however, are rarely stained or injected.

In the fang-like form, of which, strange to say, I have only found
a single specimen (fig. 16), and which corresponds to the genus Acodus
of Pander, the same structure is recognizable. But the tubuli are
rarely injected; and, since in these forms they have a direction
almost parallel to the laminz, it is difficult, if not impossible, to

1861.] HARLEY—ASTACODERMA. 547

distinguish between them. The injection, however, of a few tubuli
here and there manifests their presence and direction.

General remarks on arrangement of tubuli in Crustacean shell_—
This alteration of the relative directions of the lamine and tubuli
is what occurs in the other forms of Crustacean fragments to which
I have referred; and I also find a corresponding obliquity of their
arrangement in the spines of recent Zimuli. The same rule, in fact,
applies to both the recent and fossil integument; viz., whenever the
surface is elevated into a tubercle, the tubes have a direction a
little oblique to its surface; on the sides of a conical eminence the
tubuli lie at an acute angle; and when the eminence is included
between lines that are parallel, or nearly so, then the tubuli, as in
the spine-like Conodonts, take a direction almost parallel to the
surface. Calcareous corpuscles also occur in the Conodonts, and
are, I presume, the “ nuclei or cells,” which have been mentioned
in the description of these bodies. Iam much indebted to Professor
Huxley for two specimens of Conodonts received from Dr. Pander.
They have proved a most valuable donation, since they have enabled
me to investigate their structure and determine their identity with
my own solitary specimen.

Chemical constitution.—Chemical analyses of each of these three
classes of bodies prove that they have the same composition ; and as
far as the eye can judge of the results of operations on small quan-
tities, the proportion of their constituents appears to be equal in all.
They are composed of phosphate and carbonate of lime, the former
being, contrary to my anticipations, the more abundant constituent.
The colour is due to sesquioxide of iron.

Relationship.—Having thus determined that the bodies above
referred to, including the Conodonts of Pander, are Crustacean frag-
ments, it remains to determine, as far as possible, to what particular
genus or genera they belong.

So great is the number, and so varied the forms of the parts of a
Crustacean, that it would be quite allowable to suppose that all the
forms figured in the first four plates of Dr. Pander’s work (which
include representations of all the thirteen genera into which he has
subdivided the Conodonts) may belong to a single individual; and
the same may be said of all the forms which I have figured; but
perhaps it would be nearer the truth to assume that they have
a more distant relationship than this. May they not belong to
several or all of the orders and genera common to the strata in
which they lie?

Structure of Pterygotus.—The question may be restricted some-
what by ascertaining the structure of some of these. First, with
regard to that widely diffused genus Pterygotus. I infer that its
integument was very soft, and almost wholly composed of animal
matter, from the fact that it invariably occurs as a carbonaceous
film. We find the bony plates of Pteraspis and the testa of Tri-
lobites and Phyllopods well preserved in the mudstone-shale of the
Lower Ludlow strata; but even in the calcareous seams of the Upper

548 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

Ludlow, Pterygotus still remains as a fiimsy trace, or dark stain*.
I am not justified, therefore, in referring any of these fragments to
this genus or its allies, unless, indeed, they have such forms as are
-represented in figs. 11, 12, and 13, which may possibly be stomach-
teeth.

Structure of Trilobites—As to the Trilobites, they have a struc-
ture altogether different; from that above described. I have ex-
amined the integument of Calyimene Blumenbachii, Harpes macro-
cephalus, and Phacops latifrons: Mr. Salter kindly furnished me
with material for examining the last two genera. They all agree
in structure ; and as this is best seen in the dark-coloured Calymene
from the Lower Ludlow strata, I will take this as the type. The
integument of this genus is seen in vertical section to consist of two
distinct portions, an inner and an outer; and both are traversed by
wide straight tubes, from —)—th to -1 th of an inch in diameter,

500 :
placed at a distance of about 1 th of an inch apart, so as to be quite

isolated from each other. The outer part of the integument has a
coarsely fibrous appearance, the fibres having a horizontal direction,
and uniting obliquely to form a coarse network with narrow elliptical
meshes. I question whether this is a true structural appearance.
Magnified 300 times, this part of the integument presents obscure
indications of a finely laminated structure. In specimens from the
limestone the inner part of the integument has a prismatic struc-
ture; but I believe that this is due to crystallization of the infil-
trated carbonate of lime; for I do not observe it in specimens from
the mudstone. Moreover, the Trilobites do not appear to have
possessed articulated appendages.

Structure of Ceratiocaris—On the other hand, the structure of
the bodies in question has a great resemblance to, if not a complete
identity with, that of Ceratiocaris. In a section of one of the tail-
spines of this genus from the Upper Ludlow rock, I find both the
tubular and laminar systems well displayed; but the laminze, in-
stead of being faintly marked, are clearly and sharply defined, and
the tubuli are perhaps less crowded, and sometimes beautifully
zigzaged near their termination at the outer surface. There is
another and more general agreement between the bodies compared.
The Phyllopods of the Ludlow rocks are small, many being not much
larger than big prawns; and they possessed a very hard integu-
ment, as is proved by their remains. Further, these little animals
were very spiny, for even the tail-spines themselves were armed
with minute secondary spines disposed in longitudinal rows.

Discrimination.—Now, while their microscopic size and extreme
hardness separate the little bodies referred to in this paper from
Pterygotus and its allies, and their structure from the Trilebites,
these characters all serve to associate them with the Phyllopods,

* In the large Lesmahago specimens, in which the integument is best developed
and preserved, it appears in vertical section as a black line, the 335th of an inch
only in thickness, and no structure can be made out either in this or in a horizontal
section.

1861.] HARLEY—ASTACODERMA. 549

Indeed, I am almost convinced that many of the simple Conodonts
are really the minute spines which were attached to the tail-spines
of Ceratiocaris. Some of these are repeatedly grooved in the longi-
tudinal direction ; so are many of the Conodonts. Some tail-spines
in my possession possess rows of little oval apertures which cor-
respond to the attachment of the secondary spines, which were no
doubt moveable ; and these apertures correspond in size to the bases
of the Conodonts. Further, the Conodonts are most abundant in
those strata where, in this country at least, the Phyllopods are most
common, viz. in the Lower Ludlow.

While I would thus dispose of the spine- and tooth-like bodies, I
am much puzzled about a reference for the plates or scales. They
look at first sight like fragments of Trilobites; but, apart from their
difference of structure, the irregularity of their tuberculation and
their isolated entirety separate them from these animals. Are they
the disunited and symmetrical pieces of such a tessellated carapace
as is found in the recent genus Birgus? (figs. 18, 19).

Both the Conodonts of Pander, and the fragments which I have
described in this paper, have resemblances to the recent genera
Squilla and Limulus. In structure they exactly agree with the
latter, the carapace of which shows no differentiation into outer and
inner portions; and the whole thickness is traversed by simple, uni-
form and straight, or slightly bending tubes.

Bodies similar in form to many of those figured in tab. 1 and 2
of Dr. Pander’s work are to be found articulated with the margins of
the carapace of Limulus, and fringing the caudal appendages of some
species of Squilla. Indeed figs. 22 and 23, tab. 2, are exact representa-
tions of the posterior margin of the caudal segment of a species of
Squilla in the Museum of Comparative Anatomy at King’s College.

Astacoderma.—In order to facilitate the recognition of the bodies
mentioned in this paper, I propose to form them into one provisional
genus, from which, as each is more particularly identified, it may be
withdrawn. Astacoderma is the name I would give this genus, in
which I would also include the whole of the so-called Conodonts,
and thus give them at once a natural association, and a more appro-
priate name.

I will now briefly describe such of the more typical forms as
often occur in the Bone-bed.

ASTACODERMA TERMINALE. Pl. XVII. figs. 1 & 14.

About a line in length, conical, round or compressed and sub-
angular, hollow, the cavity usually extending about two-thirds the
length. Fig. 14 is an irregular form.

A. Bicusprpatum, Pl. XVII. figs. 2, 3, 4, 7.

Rarely exceeding a line in length, and about as broad; cusps
usually equal, vertical or oblique, each hollowed at the base into a
little conical cavity. In fig. 7 the cusps are confluent.

These two species were probably the hard extremities of limbs.

Loc. Ludlow and Norton.

900) PROCEEDINGS OF THE GEOLOGICAL society, [June 19,

A. sErRaTUM. Pl. XVII. fig. 15.

Very minute (fig. 15 does not exceed a line in its greatest di-
mension) ; the cusps are sometimes unequal and irregularly arranged ;
dark streaks indicate cavities at the bases of the cusps.

This is the Gnathodus of Pander. It is doubtless the serrated
margin of some carapace or body-ring.

Loc. Ludlow.

A, sprnosum. Pl. XVII. figs. 16a, 166.

The simple Conodont of Pander, corresponding to the genus
Acodus. Spines of Ceratiocaris, or of some Squilloid Crustacean.
Loc. A solitary specimen in the Bone- bed, Ludlow.

A. TRIANGULARE. Pl. XVII. figs. 5a & 56.

Triangular, subpyramidal, broader than long, terminated by three
cusps, two anterior, the third posterior and intermediate, more pro-
minent than the anterior; inferior surface (56) presents three de-
pressions in a general concavity, corresponding to the cusps.

Var. diffusum (fig. 6).

Var. contractum (fig. 8).

Loc. Ludlow and Norton (common).

A. pEcLINatUM. Pl. XVII. fig. 9.

Odd cusp anterior, depressed, forming the termination of a ridge
running downwards and forwards from the left posterior cusp ;
between this ridge and the right posterior cusp is a deep depression
which slopes downwards to the right side. Inferior surface concaye,
presenting a general concavity with three depressions corresponding
to cusps.

Var. depressum.

Var. expansum. Anterior cusp carried towards the right side, so
as to be nearly in front of the right posterior ; depression almost
transverse, wedge-shaped.

Var. expanso-acuminatum (fig. 10). This variety serves to con-
nect, through fig. 8 (A. triangulare, var. contractum), the last two
species described. [I am ata loss where to affix these bodies; but
the varieties delineated in figs. 8 & 10 are identical in form with
some of the stunted spines articulated to the margins of the abdo-
minal plate of Limulus.

Loc. Ludlow and Norton (frequent).

A. unpuzatum. Pl. XVI. figs. 11, 12a—12d, 18.

Cusps obsolete or nearly so; the two intervening and diverging
ridges forming a V-shaped elevation, from which the rest of the
surface declinesion, This is only a declens of variety expansum.

Var. compositum. A combination of two or even three such forms,
making a zigzag plate, bounded by a smooth, slightly elevated
margin. The under surface presents usually, but not invariably,
depressions corresponding to the elevations. This form is not un-.
like the stomach-teeth of the common Lobster.

Loc. Ludlow and Norton (not very common).

1861. ] HARLEY—ASTACODERMA. 551,

A. pranum. Pl. XVII. figs. 18, 19, 20a, 206, 20c.

Flat smooth plates, with rounded polished, or straight (some-
times polished, sometimes unpolished) edges, often as much as 7 of a
line in thickness. Superior surface slightly concave, or distinctly
included within a raised margin, occasionally marked just within
the margin with minute pits or radiated linear depressions ; inferior
surface also slightly concave, and partially bounded by a smooth
elevated border.

Var. monotuberculatum (fig. 20). Sometimes the linear depres-
sion here shown, but which is not present in the typical form, be-
comes very wide; and then the one-half of the plate is occupied by
two tubercles (fig. 19). i

Var. trituberculutum (fig. 18). Oblong or pyriform ; the superior
surface presents three pretty equal rounded tubercles, bounded in one
direction by the elevated margin of the plate. These forms resemble
the valves of some species of Beyrichia; and had they possessed a
more delicate structure and a greater concavity of one surface, one
would have been induced to refer them to these Entomostracans.

Loc. Ludlow and Norton.

This form and its varieties are very common, and make up a con-
siderable proportion of the “black scales,” of which the bone-bed
appears to be in great part composed. They may possibly belong
to some Limuloid Crustacean.

A. remiFormE. PI, XVII. fig. 17.

Flat, triangular ; superior surface convex ; inferior a little concave.
The superior surface presents near the base a transverse depression,
alternately convex and concave, apparently for ginglymoid articula-
tion.

I have met with this form twice only. It resembles some of the
little paddle-like appendages to the posterior limbs of Limulus.

Loc. Ludlow and Norton.

Dr. Volborth’s discovery of Conodonts in the Ludlow Bone-bed.—
I-would mention in conclusion, that I had, last summer, the pleasure
of showing my specimens of Conodonts from the Bone-bed to Dr. Vol-
borth of St. Petersburg, a very eminent authority in this matter,
and that he unhesitatingly confirmed the view I had taken of these
bodies, as to their being identical with Dr. Pander’s Conodonts.

, On the 30th of May last, and a short time after I had given in
my paper to the Society, I received an obliging letter from Dr, Vol-
borth, which, as it contains information not only corroborative
of some statements made in this paper, but also of general interest,
I feel that I cannot do better than transcribe.

“St. Petersburg, May 12, 1861.

« Dear Srx,—According to my promise, I beg leave to inform you
that on my return home I found hundreds of Conodonts in the de-
composed part of the bone-bed of Ludlow. They have probably
undergone metamorphic action, being white, opake, very brittle,
and not of so brilliant a lustre as ours. But they are certainly Cono-.

502 PROCEEDINGS OF THE GEOLOGICAL SOCIETY. [June 19,

donts, as Mr. Pander has been able to trace in them the same
microscopical structure, with the aid of glycerine.

«‘T found Conodonts, too, at the Isle of Oeland (Sweden), and suc-
ceeded in detecting fish-remains at the Isle of Gothland, in marls
that coat the natural divisions of the limestones of the Thorsberg, in
the south-east of the isle, close to Oestergarn. They belong to those
shagreen-scales that are so abundant in the bone-bed of Ludlow
(Thelodus, Agass.), described by Mr. Pander as Calolepis from Oesel,
and confirm the views of Sir Roderick about the younger age of the
strata in the southern part of the Island.

“ Dr. ALEXANDER VOLBORTH.”

EXPLANATION OF PLATE XVII.

Fig. 1. Astacoderma terminale; X25.
14. A. terminale, var. X15.
2, 3,4. A. bicuspidatum and varieties; X25.
7. A. bicuspidatum, var. X15.
5a. A. triangulare.
5b. A. triangulare, under surface. - X20.
6. A. triangulare, var. diffusum.
8. A. triangulare, var. contractum; X10.
9. A. declinatum; X20.
10. A. declinatum, var. expanso-acuminatum.
lla. A. undulatum: vel declinatum, var. expansum.
11}. A. undulatum, under surface. 5¢ 115),
12a. A. undulatum, var. conpositum.
13. A. undulatum, var. compositum, under surface.
126. A. undulatum, var. compositum, vertical section, x25.
12c. A. undulatum, var. compositum, vertical section, x60, showing the
tubular structure.
12d. A. undulatum, var. compositum, vertical section, x250, showing the
laminar structure (a few tubuli are injected).
15. A. serratum; X15.
16a &168, A. spinosum; X15.
17. A. remiforme; X15.
18. A. planum, var. trituberculatum; X15.
19, 20 a. A. planum, var. monotuberculatum; X15.
20 b. A. planum, var. monotuberculatum, horizontal section, X 250, showing
tubuli cut across and arranged in systems.
20 c. A. planum, var. monotuberculatum, vertical section through part of the
thickness, x 250, showing the tubuli.

*

4, On the Outsurst of a Voucano near Epp, on the Arrican Coast
of the Rep Sea. By Capt. R. L. Prayrarr, Officiating Political
Resident, Aden.

[Communicated by Sir R. I. Murchison, V.P.G.S.]
(Abstract.)

Ar Edd, lat. 13° 57’ N., long. 41° 4’ E., about half-way between

Massouah and the Straits of Bab-el-Mandel, earthquake-shocks

occurred on the night of the 7th of May or the morning of the 8th,

during about an hour. At sunrise fine dust fell, at first white, after-
wards red; the day was pitch-dark; and the dust was nearly knee-
deep. On the 9th the fall of dust abated ; and at night fire and smoke
were seen issuing from Jebel Dubbeh, a mountain aboutaday’s journey

(
ie

ee
me
oo

+.Dewilde

TH; on Stone by

ature by.!

Fram N

ASTACODERMA

bit

any

ARC

35)
fit

fi

ARE LE Leah rad AT IAN ey

ial

sl,imp

W.We

Quart Jourr Ger i] \ 10 Ve 1 XVIL} |

W West, imp
From Nature byJ'H., on Stone by G.Dewilde

AS'PACODERMA™ THE LUDLOW BONE BED

1861.] DYKES—COROMANDEL COAST. 553

inland, and sounds like the firing of cannon were heard. At Perim
these sounds were heard at about 2 a.m. on the 8th, and at long in-
tervals up to the 10th or 11th. The dust was also met with at sea;
and along the entire coast of Yemen the dust fell for several days.
Several shocks were felt on the 8th at Mokha and Hodaida.

5. Notice of the Occurrence of an Karruquaxe on the 20th of Marcu,
1861, in Mendoza, ARGENTINE ConrEDERATION, SourH AMERICA.
By C. Murray, Esq.

[Communicated by the President. ]
(Abstract.)

Ar about 3 to 9 o’clock, the first shock, preceded by a thunder-clap,
destroyed the city of Mendoza, killing (it is said) two-thirds of its
16,000 inhabitants. Altogether there were eighty-five shocks in ten
days. ‘The land-wave appears to have come from the south-east.
Several towns S.H. of Buenos Ayres felt slight shocks. No earth-
quake took place in Chile; but travellers crossing the Upsallata Pass
of the Cordilleras met with a shower of ashes ; the pass was obstructed
by broken rocks ; and chasms opened on all sides. At Buenos Ayres,
323 leagues from Mendoza, and elsewhere, it was observed in watch-
makers’ shops that the pendulums moving N. and S. were accele-
rated; those moving E, and W. were not affected,

6. On the INcrEasE of Lanp on the CoromandrL Coast.
By J. W. Dyxes, Esq.
[From a Letter* to Sir C. Lyell, F.G.S.]

Ixy the districts of the Kistna and Godavery, the land presents a paral-
lel series of ridges and hollows near the coast, not in relation to the
rivers but to the coast-line. These may have been formed by sedi-
mentary deposits similar to what are now taking place on the Coro-
mandel coast. By the strong currents alternately running N. and S.,
according to the monsoons, lines of sediment parallel with the coast
are formed; and by the occasional interference of winds and tides
dams are thrown across the hollows, and the latter soon become filled
up. These parallel bands of coast-land become, in time, upheayed
and more or less affected by atmospheric agencies.

7. The Srcrerary gave a brief account of the discovery of an ex-
posure of sandstone strata with two bands of clay full of calcareous
nodules containing plentiful remains of Coccosteus, Glyptolepis, and
other fishes belonging to the Old Red Sandstone, in a burn about
2; miles from the Manse at Edderton, Ross-shire, on the south side
of Durnoch Firth. This information was contained in a letter
from the Rey. J. M. Joass, of Edderton, communicated by Sir R. I.
Murchison, V.P.G.S.

* Dated Kottapaluam, January 17, 1861.

554

DONATIONS
TO THE

LIBRARY OF THE GEOLOGICAL SOCIETY.

From April 1st to June 30th, 1861.

I. TRANSACTIONS AND JOURNALS.
Presented by the respective Societies and Editors.

American Journal of Science and Arts. Second Series. No. 70.
July 1857. From Prof. B. Silliman, For.M.G.S.

C. U. Shepard and F. A. Genth.—Minerals of the Canton Mine,
38, 133.

J. Hall.—Cretaceous Strata of the United States, 72.

J. D. Dana.—Fourth Supplement to Dana’s ‘ Mineralogy,’ 183.

C. U. Shepard.—Meteoric Stone which fell in Tennessee, Aug. 5,
1855, 134.

J. W. Mallet.—Separation of Magnesia and Lithia, 187.

Wohler.—New Oxide of Silicon, 140.

Brunner.—Manganese, 140; Frémy, Chromium, 141.

H. Ste-Cl. Deville.—Preparation of the Elements, 141.

O, M. Lieber.—Geological Survey of South Carolina, 145.

J. S. Newberry.—New fossil Fishes from the Devonian Rocks of
Ohio, 147.

F. B. Meek and F. V. Hayden.—New fossil species of Mollusca, 149,

H. G. Bronn.—Proportion of Bivalves of different Geological Ages,
150.

J. Tyndall and H. C. Sorby.—Slaty Cleavage, 160.

Filtration through Sand, 157; Density of the Earth, 158.

—. Vol. xxxi. No.92. March 1861.

A. Guyot.—Appalachian Mountain System, 157 (Map).

J. P. Cooke.—Dimorphism of Arsenic, Antimony, and Zine, 191.

J. M. Safford.—Upper Silurian Beds of Western Tennessee, 205.

J. Barrande, E. W. Logan, and J. Hall—Taconic and Quebec
Groups of Rocks, 210.

S. D. Hayes.—A new Lead-salt, 226,

DONATIONS, 555

American Journal of Science and Arts. No. 92 (continued).

F, V. Hayden and W. F. Raynolds.—Geology of the Country about
the Head-water of the Missouri and Yellow Stone Rivers, 229.

W. Cribbs.—Atomic Weights of the Elements, 246.

J. L. Smith.—Three new Meteorites, 264.

A. Delesse.-—Metamorphism and Pseudomorphism, 273.

F. H. Storer.—Alloys of Copper and Zinc, 286.

J. W. Dawson.—Fossils of the Coal of Nova Scotia, 290,

J. Hall’s ‘Contributions to Geology,’ noticed, 293.

——. Vol. xxxi. No. 93. May 1861.

E. T. Doane.—The Atoll of Ebon in Micronesia, 318.

F. J. Pictet.—The Quaternian or Diluvian Period, 345.

J. Schiel.—The presence of Phosphoric Acid in Igneous Rocks, 353.

G. J, Brushe.—Ninth Supplement to Dana’s ‘ Mineralogy,’ 354.

E. Hitcheock.—Conversion of certain Conglomerates into Talcose
and Micaceous Schist and Gneiss, 372.

T. 8S. Hunt.—Some Points in American Geology, 392.

F, H. Storer.—Alloys of Copper and Zine, 428.

L. Lesquereux.—Botanical and Paleontological Report on the Geo-
logical State Survey of Arkansas, 431.

O. Heer.—Fossil Leaves of Nebraska, 435.

W. B. Rogers.—Elongate Form and parallel Arrangement of the
Pebbles in the Newport Conglomerate, 440.

T. S. Hunt.—Chloritoid from Canada, 442.

J. Phillips’s ‘ Life on Earth,’ noticed, 444.

C. U. Shepard.—Catalogue of his Collection of Meteoric Stones and
Meteoric Irons, 456.

Assurance Magazine. Vol.ix. Part 5. No. 43. April 1861.3
Atheneum Journal. Nos. 1745-1757.

Notices of Meetings of Scientific Societies, &c.

W.S. Symonds’s ‘Old Bones,’ noticed, 527.

Obituary Notice of J. 8. Henslow, 696.

Palmieri.—Vesuvius, 703.

Wilson and Geikie’s ‘Memoir of Edward Forbes,’ noticed, 756.
H. F. A. Pratt’s ‘The Genealogy of Creation,’ noticed, 860.

D. Page’s ‘The past and present Life of the Globe,’ noticed, 865.

Berlin. Monatsberichte d. Konig. Preuss. Akad. d. Wissensch. Re-
gister vom Jahre 1836 bis 1858. 1860.

‘__—., Monatsberichte for 1860. 1861.

Beyrich.—Ueber Semnopithecus Pentelicus, 549.

Bunsen. —Entdeckung eines dem Kalium ahnlichen Metalls, 221.

Ehrenberg.—Meteoreisen und -steinen aus Nordamerika, &c., 517.

Heintz.—Boracit, 466.

Rammelsberg.—Ueber das Verhalten der aus Kieselsiure bestehen-
den Mineralien gegen Kalilauge, 758.

G. Rose.—Vorkommen der Diamanten in Brasilien, 137.

Ueber die heteromorphen Zustiinde der kohlensauren Kalk-
erde, 365.

H. Rose.—Ueber die unterniobsauren Salze, 710.

R. Schneider.—lIsomorphie der Jodantimon mit Jodwismuth, 56.

Ueber Wismuth- und Antimonjodosulfuret, 57, ia

556 DONATIONS.

Berwickshire Naturalists’ Club. Proceedings, 1861.
R. Carr.—Anniversary Address, Sept. 13, 1860, 157. -
J. Hardy.—Fossil Antlers of Roebuck, Megaceros, and Red-deer at
Coldingham, 206, 214 (plate).

Brussels. Annuaire de l’Académie Royale des Sciences, des Lettres
et des Beaux Arts de Belgique. 1861.

——. Bulletins de l’Acad. Roy. 29™e Année, 2me Sér. Vol. ix.
1860.

Scohy.—Sur une découverte d’ossements fossiles & Lierre, 405, 436
(plate).

Vol. x. 1860.

Van Beneden.—Discours prononcée 16 Décembre, 709.

Raemdonck, Nyst, &c.—Sur ossements fossiles trouvés dans les en-
virons de St.-Nicholas, 401.

Montigny.—Sur des débris d’animaux fossiles trouvés prés de Ni-
velles, 450.

Dewalque et autres.—Sur les fouilles faites & Anvers, 508, 599.

Malaise De Koninck, et d’Omalius.—Sur des ossements humains
fossiles, et sur quelques silex taillés, 511, 514, 538 (plate).

. Mémoires couronnés et autres mémoires publiés par l’Acad.
Roy. de Belgique. Collection in 8yo. Vol. x. 1860.

A. Perrey.—Sur les Tremblements de Terre in 1857, avec Supplé-
ments pour les années antérieures.

Mémoires de l’Acad. Royale de Belgique. Vol. xxx. 1861.

Caen. Bulletin de la Soc. Linnéenne de Normandie. Vol. v. Année
1859-60.
Perrier.—Sur quelques fossiles recueillis sur la route des champs
St.-Michel, 89.
De Caumont.—Sur quelques fossiles recueillis dans le lit de la
Dive, 91.
Sur les bords de la Mer Jurassique du sud-est de la France,

92.

E. Deslongchamps.—Sur un corps fossile, 111 (pl. x. figs. 5-8).

E. E. Deslongchamps.—Sur quelques Gastéropodes fossiles des ter-
rains jurassiques, 119 (plate).

E. Deslongchamps.—Sur une nouvelle coupe générique de gastéro-
podes fossiles, nommée Eucyclus, 138 (plate).

i. Hébert et E. E. Deslongchamps.—Sur les fossiles de Montreuil-
Bellay, 153 (9 plates).

De Brébisson.—Empreintes de corps organisés sur une roche Cam-
brienne, 244 (plate).

Caleutta. Asiatic Society of Bengal. Journal. New Series. No.105.
1860, No. 4.
W. T. Blanford.—Rocks of the Damuda Group of Raniganj, 352.
H. J. Carter—Geological specimens from the Persian Gulf, &c., 359.
No. 106. 1861, No.1.
H. B. Medlicott.—The Sub-Himalayan Rocks, 22.

DONATIONS. Bah

Canadian Journal. New Series. No. 32. March 1861.

D. Wilson.—Presidential Address, January 13, 1861, 101.

E. Billings.—Devonian Fossils of Canada West, 158 (figures).

E. J. Chapman.—Minerals and Geology of Canada, 149.

Hi. Y. Hinde’s ‘ Narrative of the Canadian Red River Exploring ix-
pedition,’ &¢., noticed, 175.

J. Hall’s ‘ Contributions to Paleontology,’ 1860, noticed, 187,

Chemical Society. Quarterly Journal. No. 53. Vol. xiv. Part 1.
April 1861.

H. M. Noad and A. Voelcker.—Analysis of the Saline Water of
Purton, near Swindon, 43, 46.
F. Field.—Carbonates of Copper, Nickel, and Cobalt, 48, 70.

Cherbourg, Mémoires de la Soc. Imp. des Sc. Nat. de. Vol. vii.
1859. 1860.

Jouan.—Sur les iles basses et les récifs de corail du Grand-Océan,
148,

—. Sur le Guano des iles Chinchas, 364.

Bonissent.—Découverte de Fossiles & Couville, 372.”

Critic. Vol. xxii. Nos. 561-573.

Notices of Meetings of Scientific Societies, &c.
Obituary Notice of J. S. Henslow, 706.
Wilson and Geikie’s ‘ Memoir of E. Forbes,’ noticed, 755.

Dublin. Royal Irish Academy. Transactions. Vol. xxiv. Part 1.
1860.

G. J. Stoney.—Rings seen in fibrous specimens of Calc-spar, 31.

Empire, the (Sydney). No. 2911. January 28, 1861.
Australian Gold-fields, 2.

Falmouth. Cornwall Polytechnic Society. 28th Annual Report.
1860.

R, Q. Couch.—Mortality of Cornish Miners, 18.
H. C, Salmon.—Origin of Crystalline Rocks, 97.

Geologist. Vol.iv. No.40. April 1861.

J. W. Salter.—Coal, 121.
C. Hutton.—The Darwinian Theory, 130.
J. Powrie.— Cephalaspides of Forfarshire, 137,
R. Lightbody.— Cephalaspides of Worcestershire, 140.
A. Marston.—Cephalaspides from near Ludlow, 141.
Foreign Correspondence, 142.
V. Lipold.—Silurian “Colonies” of Bohemia, 142.
W. W. Woods.—Minerals of the Philippines, 143.
Notices of Societies, 145.
Notes and queries, 157.
Heusser and Claraz.—Diamond-workings of Brazil, 163.
G. R. Vine.—Geology of Athlone, 169.
J. F. Whiteaves.—Oolitic Echinodermata of Oxford, 174.
Reviews, 176.
yOL, XYII.—PART I. 2P

558 DONATIONS.

Geologist. Nos. 41,42. May and June 1861.

J. W. Salter.—Coal, 177, 229.

F. W. Hutton.—The Darwinian Theory, 183.

G. E. Roberts.— Cephalaspis and Pteraspis, 189.

C. Moore.—Terebella, and some new Brachiopoda, 190.
Fossil Chitons, 222.

Iceland, 225.

G. W. Stow.—Geology of Sundays River, South Africa, 238.
F. Drake.—Human Remains in the Vale of Belvoir, 246.
Foreign Correspondence, 194, 247.

Proceedings of Societies, 206, 256.

Notes and Queries, 212, 258.

Reviews of Books, 268.

Hanau, Jahresbericht der Wetterauer Gesellschaft fur d. gesammte
Naturkunde zu. 1861.

R. Ludwig.—Ueber Bodenschwankingen im Gebiete des untern
Mainthales wihrend der Periode der Quartarbildungen, 1.

,. Blum.—Die in Wetterau vorkommenden Pseudomorphosen, 15.

—. Neue Fundorte von Mineralien in der Wetterau, 26.

—. Roesslerit, em neues Mineral, 52.

Heidelberg, Verhandlungen des nat.-med. Vereims zu. Vol. i.
Part 2.

R. Blum.—Ueber eine besondere Art der Ausfiillumg yon Blasen-
raiumen in Mandelsteinen, 82.

—. Ueber Pseudomorphosen und Einschliisse von Mineralien in
Mineralien, 87.

India, Geological Survey of. Annual Report. 4th year. 1859-
60. 1860.

Institution of Civil Engineers. Proceedings. Session 1859-60,
Nos. 2-20; and Session 1860-61, Nos. 1-25.
C. E. Amos.— Waterworks at Trafalear Square.
F. Braithwaite.—Rise and Fall of the River Wandle, &c.
J. Murray.—The North Sea, or German Ocean; its Estuaries,
Rivers, and Harbours.

Jena. Nova Acta Acad. Cs. Leop.-Carol. Germ. Nat. Cur. Vol.
xxvil. (3rd Ser. Vol. viii.). 1861. (Comprising the Leopoldina,
Heft ii.)

Linnean Society. Journal of the Proceedings. Vol. vy. Nos. 19, 20.

—. ——. 2nd Supplement, to Vol. v., Botany. May 24, 1861.

——. Charter and Bye-laws. 1861.

—. Transactions. Vol. xxii. Partl. 1860.

—. List of Fellows. 1860.

DONATIONS, 559

Literary Gazette. Vol. vi. Nos. 147-156.

Notices of Meetings of Scientific Societies, &e.

K. Scherzer’s ‘ Voyage of the Novara,’ noticed, 435.

D. Page’s ‘The Past and Present Life of the Globe,’ noticed, 534.
Wilson and Geikie’s ‘Memoir of Edward Forbes,’ noticed, 563.
J. Cumming’s ‘Isle of Man,’ noticed, 582.

London. International Statistical Congress, the Fourth Session.
Programme. 1860.

R. Hunt.—Statistics of Mineral Produce, &c., 85.
Mortality of Miners, 55,

——. ——. Report of the Proceedings. 1861.

R. Hunt.—Statistics of Miners, 306.
—. Mortality of Miners, 309.

London, Edinburgh, and Dublin Philosophical Magazine. 4th Series.
Vol. xxi. Nos. 140-142. April-June 1861. from Dr. W.
Francs, F.GS.

W. Crookes.—A new Element, probably of the Sulphur group, 301.

J. D. Smithe.—Gravel of the Punjab, 505.

T. H. Huxley.—Pteraspis Dunensis, 305.

W. Whitaker.—Chalk-rocks of Wilts, Berks, &c., 306.

R. I. Murchison and A. Geikie——Western and Central Islands,
306.

. Coincidence between Stratification and Foliation in the
Highlands, 308.

R. Harkness.—Silurian Rocks in the Highlands and N. W. Ireland,
308.

F. Drew.—Hastings Sand, 309.

J. W. Kirkby.—Permian Rocks and Fossils of South Yorkshire,
310.

D, Campbell.—Avrsenic and Antimony in Streams and Rivers, 318.

F. yon Kobell.—Dianic Acid, 415.

H. J. Chapman.—Drift Deposits of Western Canada, 428.

A. Daubrée.—Capillary Infiltration, 479.

—. —. No. 143. Supplement. June 1861.

C. Bunbury.—Fossil Plants from Nagpur, 536.

S. Hislop.—Plant-bearing Sandstones of Central India, 586.

W. B. Clarke.—Age of the Coal-rocks of New South Wales, 537.
T. H. Huxley.—Reptilian Remains from Bengal, 537.

J. Hector.—Geology of the Rocky Mountains, 537.

A. Gesner.—Movements of the Land in North America, 539.

London Review. Vol. 11. Nos. 40-52. April-June 1861.

Notices of Scientific Societies’ Meetings, &c.

D. Livingstone.—Victoria Falls, Tete, &c., 476.
Spectrum-analysis of Metals, 521.

D. Walker.—Geology of the Arctic Regions, 537.
Mosaic Cosmogony, 585.

Spectrum-analysis, 649, 766.

560 DONATIONS.

London Review. Vol.ii. Nos. 40-52. April-June 1861 (continued).

R. Fitzroy.—Stone-tools in Drift, 638.
Freshwater Spring in the Sea off Florida, 664.
Carbon and its combinations and products, 732.

Longman’s Monthly List. June 1, 1861.
——. Notes of Books. No. 25. May 1861.

Manchester Geological Society. Transactions. No.5. 1861.

J. Dickinson.—Locks for Miners’ Safety-lamp3, 57.

Petroleum in Coal-mines, 62.

P. Higson.—Outbursts of Fire-damp in Coal-pits, 64.

P. Cartellieri.—The Francis Well at Eger influenced by atmospheric
pressure, 68.

J. Taylor.—Geology of Castleton, 73.

Mechanics’ Magazine. NewSeries. Vol.v. Nos. 119-131.

Notices of Meetings of Scientific Societies, &c.
Ventilation of Coal-mines, 230, 261.
Fremy.—Composition of Steel, 364, 412.

R. Musket.—Chemistry of Steel, 371, 386, 405, 418.
J. R. Liefchild.—Ventilation of Coal-mines, 379.

Melbourne (Victoria). Mining Surveyors’ Reports. No. 23.
March 1861.

Milan. Atti del Reale Istituto Lombardo di Scienze, &e. Vol. i.
Fase. 4-9. 1860-61.

Memorie del Reale Istituto Lombardo, &c. Vol. viii. (Vol.
ii. of the 2nd series), fasc. 4. 1861.

Munich. Sitzungsberichte Kon. bayer. Akad. Wissensch. 1860.
Hefte 4&5. 1860. Zu Minchen.

A. Wagner.—Ueber den gegenwirtigen Standpunct der Theorien
der Erdbildung nach ihre geschichtlichen Entwickelung in den
letzten fiinfzig Jahren, 375.

Vogel.—Ueber die Filllung des schwefelsauren Manganoxyduls durch
Silberoxyd, 659.

A. Wagner und Lindermayer.—Ueber die fossilen Knochenreste yon
Pikermi, 647.

New York. The Second Annual Report of the Trustees of the

Cooper Union for the Advancement of Science and Art. January
1, 1861.

New Zealand Examiner. No. 16.

Paris. Annales des Mines. 5™e¢ Sér. Vol. xviii. Livr. 5 et 6 de
1860.

A. Delesse.—Recherches de l’azote et des matiéres organiques dans
l’écorce terrestre, 219,

DONATIONS. 561
Paris. Annales des Mines. 5™° Sér. Vol. xviii. Livr. 5 et 6 de
1860 (continued),

H. Ste.-Cl. Deville et H. Debray.—De la métallurgie du platine et
des métaux qui ’accompagnent, 326.
B, von Cotta.—Minéraux des filons metalliféres de Freiberg, 649.

Vol. xix. Livr. 1 de 1861.

A, Daubrée.-—Percement de certaines roches trés dures, 25.

—
°

Bulletin de la Société Géologique de France. Deux. Sér.
Vol. xvii, Feuil. 1-6. 1861.

Ed. Piette.——Sur un nouveau genre de gastéropodes (Lvelissa), 14.

Tournal.—Sur la présence, dans les cavernes, d’animaux d’espéces
perdues, 15.

Gosselet et Delanotie.—Sur les terrains primaires de la Belgique et
du nord de la France, 18, 33.

Ch. Lory.—Sur la constitution stratigraphique de la Haute-Mau-
rienne (pl. 1), 34.

Alph. Fayre.—Sur la Structure des montagnes qui constituent le
versant nord de la Maurienne (pl. 2.), 47.

J. Delbos.—Sur VPostéologie comparée des Ours vivants et fossiles, 53.

Loustau.—Coupe du terrain traversé par la ligne de Chauny a Saint-
Gobain, 77.

Ed. Hébert.—Gisement des couches marines de Sinceny (Aisne), 77.

Buteux.—Sur des bancs du diluvium avec débris d’espéces d’ani-
maux perdus superposés & Amiens & des couches de tourbe, 79.

Em. Goubert.—Coupes dans les marnes de Saint-Ouen, 80.

Marcel de Serres.—Sur la troncature normale des coquilles des mol-
lusques gastéropodes, etc., 87.

Anca.—Sur existence de l’Elephas africanus en Sicile, 90.

Albert Gaudry.—Sur quelques os gigantesques provenant des nou-
velles fouilles entreprises 4 Pikermi (Gréce), 91.

——. ——. Vol. xvii. Feuil. 7-12. 1861.

Ed. Hébert.—Sur la mer jurassique et les théories imaginées pour
rendre compte de ses déplacements, 97.

A. Laugel.—Sur le Blatterstein du Harz, 103.

E. Dumortier.—Sur le Cirrus Fourneti (Thiolliére) (pl. 3), 106.

Daubrée.—Sur les zéolithes formées dans un béton romain par les
eaux thermales de Luxeuil (Haute-Sadne), 108.

Ch. Ste-C. Deville.—Sur le tremblement de terre éprouvé aux An-
tilles le 8 février 1843, 110.

A. Boué.—Sur Vorigine de la Société géologique de France, 150.

H. Coquand.—Rapports entre les groupes de la craie moyenne et de
la craie supérieure de la Provence et du sud-ouest de la France,
133.

Deshayes.—Analyse d’un travail de M. Ed. Suess sur les Brachio-
podes de la collection de Vienne, 165.

Ed. Suess.—Faune du bassin néo-tertiaire de Vienne, 168.

Th. Ebray.—Stratification de la craie moyenne comprise entre la
Loire et le Cher, 176.

Bertrand de Lom.—Sur les nombreuses espéces minérales découvyertes
dans les cing départements volcaniques de la France, 192.

562 DONATIONS,

Paris. Bulletin de la Société Géologique de France. Deux. Ser.
Vol. xviii. Feil. 13-21. 1861 (continued).

A. Daubrée.—Sur la possibilité d’une infiltration capillaire au travers

des matiéres poreuses, &c., 193.
_J. Barrande.—Sur la faune primordiale et le Systeme taconique en

Amérique (pl. 4 et 5), 203.

L. Saemann.—Sur l’unité des phénoménes géologiques dans le sy-
stéme planétaire du soleil, 522.

F. Cailliaud.—Sur l’existence de la faune troisiéme silurienne dans
le nord-est du département de la Loire-Inférieure, 330.

. Mémoires de la Société Géologique de France. Deux. Série.
Vol. i. pt. 2. 1846.

Thorent.—Sur la constitution géologique des environs de Bayonne,
181 (plate).

J. Cornuel.—Deseription des entomostracés fossiles du terrain cré-
tacé inférieur du département de le Haute Marne, 193 (plate).

A. Viquesnel.—Journal d’un yoyage dans la Turquie d’Europe, 207

map).

B, Studer.—Sur la masse des montagnes entre la route du Simplon
et celle du Saint-Gothard, 505 (map and plate).

A, Leymerie.—Sur le terrain 4 nummulites (épicrétacé) des Cor
biéres et de Ja Montagne Noire, 337 (map and 5 plates).

Vol. iv. Pt. 2. 1852.

L, Bellardi, &e.—Catalogue raisonné des fossiles nummulitiques du
Comte de Nice, 205 (11 plates).
A, Delesse.—Recherches sur les roches globuleuses, 301 (4 plates).

Ee agli ot ede i

H. Coquand.—Description géologique de la province de Constantine,
1 (4 plates).

J. Haime.—Description des bryozoaires fossiles de la formation juras-
sique, 157 (4 plates).

O. Terquem.—Paléontologie du systéme du lias inférieur du grand-
duché de Luxembourg et de Hettange, du dép. de la Moselle, 223
(15 plates).

E. Hébert.—Tableau des fossiles de la craie de Meudon, 345 (3 plates).

—_——_
«

—. —. Vol.vi. 1856-9.

J. Duroche.—Constitution géologique de la Norvége, de la Suéde,
et de la Finlande, 1 (2 maps and 1 plate).

L. D’Archiac.—Etudes géologiques d’une partie des départements de
lAude et des Pyrénées-orientales (les Corbiéres), 209 (map and
3 plates).

——. ——. Vol.vu. Mém. No.1. 1860.
J. Martin.—Paléontologie stratigraphique de l’infra-lias, 1 (8 plates).

Comptes Rendus des Séances de l’Acad. des Sciences. Tables
du tome li.

Geof. St.-Hilaire.—Classification anthropologique et zoologique, 432.

DONATIONS. 563

Paris. Comptes Rendus des Séances de l’Acad. des Sciences. Tables
du tome li. (continued).

Delesse.—Recherche de l’azote dans les substances minérales, 286, 405.

Nicklés.—Relations d’isomorphisme entre le bismuth et l’antimoine,
1097.

Bechamp.—Cuivre dans les eaux de Balaruc, 215.

Moissenet.—Du dosage de l’étain dans ses minerais, 205.

Thomassy.—Sur le delta du Mississippi, 133,

C. Méne.—Sur le groupe de la Montagne Noire (Aude), 31.

Durocher.—Recherches sur les syst¢mes de montagnes de l’Amérique
Centrale, 45.

Etudes hydrographiques et géologiques sur le lac de Nica-
ragua, 118.

S. Gras.—Opposition entre l’ordre stratigraphique des couches et
leurs caractéres paléontologiques, 108.

De Chancourtois.— Distribution des minerais de fer, 414.

Phipson.—Roche récemment formée sur le littoral de la Flandre, 419,

Gaudry.—Couche fossilifére de Pilermi, 500.

Pissis.—Travaux géologiques et géodésiques exécutés au Chili, 603.

Poucel.—Important gisement de minerai d’argent dans l’Ambato
(Confédération Argentine), 604.

E. Robert.—Recherches sur les matiéres, notamment les pierres, qui
ont été travaillées par les premiers habitants des Gaules, 660.

Engelhardt.—Formation de la glace au fond de l’eau, 28,

Maille-—Moyen @’amplifier les marées & l’embouchure des riviéres,
762.

Aynoux.—Sur un minerai de Camboge contenant du plomb, du cuivre,
et de l’argent, 455.

Méne.—Sur une nouvelle espéce de cuivre gris, la fournérite, 465.

Pisani.—Analyse de la elaubérite de Varengeville prés Nancy, 731.

Gaudry.—Résultats des nouvelles fouilles faites 4 Pikermi (Attique),
457.

—. Lettre annoncant l’envoi de ces fossiles—Détermination géo-
logique de la couche qui les recélait, 500, 502.

——. Piéces apportées de Gréce, 634, 780.

—. Fémur, humérus et autres os des membres d’un grand mam-
mifére supposé étre un Dinotherium, 802.

Sur une machoire de Metarctus et de Leptodon provenant
du gisement fossilifére de Pikermi, 926.

Gervais.—Sur la présence du grand daim et du renne parmi les fos-
siles des environs de Montpellier, 654.

A. Edwards.—Sur les crustacés fossiles des sables de Beauchamp, 92.

Bordas.—Certains faits de paléontologie, 897.

Damour.—Sur les sources thermales et les fumeroles du cone de la
Soufriére (Guadaloupe), 561.

Prost.—Secousses ressenties 4 Nice du 3 au 12 juin 1860, 67.

Terreil.—De la présence du vanadium dans les argiles de Forges-
les-eaux et de Dreux, 94.

——. Comptes Rendus de l’Acad. Sc. 1861. Prem. Semestre.
Vol. li. Nos. 6-20.

Philadelphia Academy of Natural Sciences. Proceedings. 1861.
pp. 1-64.

W. M. Gable-—American Cretaceous Brachiopoda, 18.
Photographic Society. Journal. Nos. 108-110. April—June, 1861.

564. DONATIONS,

Puy, Annales de la Société d’Agriculture, Sciences, Arts, et Com- ~
merce du. Vol. xxi., 1857-58. 1861.

Quarterly Journal of Microscopical Science. New Series. No. 1.
January 1861.

Royal Geographical Society. Proceedings. Vol. v. Nos. 1, 2.

J. Rae.—Feeroes and Iceland, 80.
J. W. Tayler.—Fiords of South Greenland, 90.

Royal Horticultural Society. Proceedings. Vol.i. Nos. 23-25.
April-June, 1861.

Royal Society of London. List of Fellows. 30th November, 1860.
—. Proceedings. Vol. xi. No. 43.

——. Philosophical Transactions. Vol. cxlix. Part I. 1859.

W. 5B. Carpenter.—Researches on Foraminifera, Part III. (Penero-
plis, Operculina, and Amphistegina), 1 (6 plates).

Rt. Owen.—Remains of a gigantic Land-lzard (Megalania prisca)

- from Australia, 45 (2 plates).

Vertebral Characters of the Pterosauria, 161 (plate).

——._ Fossil Mammals of Australia, Part I. Thylacoleo carnifex, 309.

B. C. Brodie.—Atomic weight of Graphite, 249.

J. 'Tyndall.—Physical Phenomena of Glaciers, 261.

Veined Structure of Glaciers, 279.

—— ——. Vol. exlix. Part Hl. 1860.

J. H. Pratt.—Deflection of the Plumb-line in India, 745.
Influence of the Ocean on the Plumb-line in India, 779.
R. Owen.—The Megatherium, Part V., 809 (6 plates).

—— —. Vol. cli. Part I. 1860.
A. Matthiessen.—Specific Gravity of Alloys, 177.

Society for the Suppression of Mendicity. 43rd Report. 1861.
Society of Arts. Journal. Vol. ix. Nos. 437-449.

J. Milligan.—Tasmania, its Character, Products, and Resources, 377.
J), Campbell.—Economiec History of Paraffine, 393.
Consular Information (Mines of Honduras, Mexican Copper-mines,
Minerals of Siam), 549, 578.
Teign -Naturalists’ Field-club. Report of the Proceedings, 1860,
1861. ,

Vienna. Jahrbiicher der k.-k. Central-Anstalt fir Meteorologie und
Erdmagnetismus. Vol. vii. Jahrgang 1855. 1860.

Sitzungsberichte d. k. Akad. d. Wissensch., math.-naturw.
Classe. Vol. xlii. Nos. 22-28. 1861.

A. Schrauf.—Bestimmung der optischen Constanten krystallisirter
Korper, 107 ( plate).

F. Rolle-—Ueber einige neue oder wenig gekannte Mollusken-Arten
aus Secundir-Ablagerungen, 261 (plate).

DONATIONS. 565

Vienna. Sitzungsberichte d. k. Akad. d. Wissensch. (continued).

W. Haidinger.—Die Mereoritenfalle von Quenggonk bei Bassein in
Pegu und Dhurmsala im Punjab, 301.

——, Ueber das Meteoreisen von Tula, 507.

A. E. Reuss.—Beitriige zur Kenntniss der tertiaren Foraminiferen-
Fauna (die Foraminiferen des Crags von Antwerpen), 355 (2 plates).

Th. Wertheim.—Analyse des I[ranz-Josephs-Bades “ Tuffer” in
Siid-Steiermark, 479.

G. Tschermak.—Analyse des Granates von Dobschau, 582.

E. Suess.—Ueber die secundaren Brachiopoden Portugals, 589 (plate).

Warwickshire Naturalists’ and Archeologists’ Field-club. 1860.

P. B. Brodie.—Igneous Rocks of the South Staffordshire Coal-field, 5.
Geology of Bewdley, Trimpley, &c., 12.

Yorkshire Philosophical Society. Annual Report for 1860. 1861.

Zoological Society. Proceedings, 1860, Part III. 1861.
A. Newton.—Bones of Dodo from the Mauritius, 443.

II. PERIODICALS PURCHASED FOR THE LIBRARY.

Annals and Magazine of Natural History. 3rd Series. Vol. vii.
Nos. 39-42. March—June 1861.

H. Seeley.—Red Limestone of Hunstanton, 233.

. New Species of fossil Gasteropods from the Upper Greensand
of Cambridge, 281 (plate).

. New Fossil Echinoderns from Cambridge, 365.

M. Schultze.—Cornuspira and the Foranunifera, 306.

J. Phillips’s ‘ Life on the Earth,’ noticed, 399.

C. C. Blake.—Discovery of Macrauchenia in Bolivia, 441.

Edinburgh New Philosophical Journal. New Series. No.26. Vol. xiii.
No. 2. April 1861.

W. J. Henwood.—Silver produced in Cornwall, 173.

W.S. Symonds. Railway-cuttings and Tunnels between Worcester
and Hereford, 204 (plate).

J. W. Dawson’s ‘ Archaia,’ noticed, 291.

T. Oldham.—Slate in India, 333.

Institut, ’. IT Section. Nos. 1420-1438.

——. Il*Section. Nos. 302-305.
Notices of Meetings of Scientific Societies, &ec.

Leonhard und Bronn’s Neues Jahrbuch fir Min., &. Jahrg. 1861,
2tes Heft.

J. Noggerath.—Das Gediegen-Blei von Madera, 129.

Th. Scheerer.—Ueber die Krystall-Form des Gadolinits, 134 (plate).

A. Knop.—Ueber Pseudomorphosen einer pisolitischen Substanz nach
Cordierit aus dem Granit von Heidelberg, 142.

S. Suess.—Numerische Uebersicht der Klasse der Brachiopoden, 154.

Letters: Notices of Minerals, Geology, and Fossils.

566 DONATIONS.

III. GEOLOGICAL AND MISCELLANEOUS BOOKS.
Names of Donors in Italies.

Annales Hydrographiques, recueil d’avis, instructions, documents
et mémoires relatifs 4 ’? Hydrographie et 4 la Navigation. Tome
16™°, année 1859, 1859; tome 17™°, année 1860, 1860; tome
18™°, année 1860, 1860. From the Dépot de la Marine.

Annuaire des Marées des Cotes de France pour an 1861. Par A. M.
R. Chazallon et L, Gaussin. 1860. From the Dépét de la Marine.

Barrande, J. Documents anciens et nouveaux sur la faune pri-
mordiale et le Systeme Taconique en Amérique. 1861.

, W. Logan, and J. Hall. Correspondence on the Taconic
System and the age of the Fossils found in Northern New Eng-
land. 1861. From the Editors of Silliman’s Journal.

Bell, T. Mineral Veins: an enquiry into their origin, founded on a
study of the Auriferous Quartz-veins of Australia. 1861.

Catalogue chronologique des Cartes, Plans, Vues de Cotes, Mémoires,
Instructions Nautiques, &c. 1860. From the Dépot de la Marine.

of the Philosophical Apparatus, Minerals, Geological Speci-
mens, &c. in the possession of Dr. Daubeny. 1861. From Dr.
Daubeny, F.GS.

par ordre géographique des Cartes, Plans, Vues de Cotes,
Mémoires, Instructions Nautiques, &c. 1860. FHrom_the Dépot de
la Marine.

Verzeichniss der Bibliothek und Kartensammlung des Pro-
fessors Ritters, &c. Dr. C. Ritter in Berlin. II. Theil: Land-.
kartensammlung. 1861. From the Publishers.

Catalogues of the Natural History Collections in the British Museum.
From the Trustees of the British Museum.

List of Osteological Specimens. 1847, 12mo.

Catalogue of Mammalia. Part 1. Cetacea. 1850, 12mo. (plates).

Part 2. Seals. 1850. 12mo. (woodcuts).

Part 3. Ungulata Furcipeda. 1852. 12mo.

List of Mammalia. 1843. 12mo. (plates).

and Birds of Nepal, presented by B. H. Hodgson, Esq. 1846. 12mo.

Catalogue of Mammalia and Birds of New Guinea. 1859. 8vo.

of the Birds of the Tropical Islands of the Pacific. 1859. 8yvo.

— of the Genera and Subgenera of Birds. 1855. 12mo.

List of Birds. Part 1. Accipitres. 2nd edition. 1848. 12mo.

——. Part 2. Passeres. Sect. 1. Fissirostres. 1848. 12mo.

—. Part 3. Sect. 1. Ramphastide. 1855. 12mo.—Sect. 2. Psittacide.
1859. 12mo.

. Part4. Columbe. 1856. 12mo.

Catalogue of Shield Reptiles. Part 1. Testudinata (Tortoises) (with plates).
1855. 4to.

— of Reptiles. Part 1. Tortoises, &c. 1844. 12mo.

DONATIONS. 567

Catalogues of the Natural History Collections in the British Museum
(continued).

Catalogue of Reptiles. Part 2. Lizards. 1845. 12mo.
Part 3. Snakes. 1849. 12mo
of Colubrine Snakes. 1858. 12mo.
— of Amphibia. Part 2. Batrachia Gradientia, &ce. 1850. 12mo.
(plates).
of Batrachia Salientia. 1858. 8vo. (plates).
List of Fish. Part 1. Chondropterygii. 1851. 12mo. (plates).
Catalogue of Fish, collected and described by L. T.Gronow. 1854. 12mo.
of Lophobranchiate Fish. 1856. 12mo, (plates).
of Apodal Fish. 1856, 8vo. (plates).
—— of Acanthopterygian Fishes. Vol.i., 1859, 8vo.; Vol.ii., 1860, 8vo.
—— of Lepidopterous Insects. Part 1. Papilionide, &. 1856. 12mo.
——. Part 2. Hrycinide, &e. 1847. 12mo.
—. Part 5. Appendix to HEtpulioms ea, Erycinidex, &e. 1848. 12mo.
——. Part 1. Papilionide. 1852. 4to. (coloured plates).
List of Lepidopterous Insects. Parts 1 to 7. Lepidoptera Heterocera.
1854-1856. 12mo.
——. Part8. Sphingide. Parts9to15. Noctuide. 1856-1858. 12mo.
——. Part 16. Deltoides. 1858. 12mo.
—. Parts 17 to 19. Pyralides. 1859. 12mo.
Parts 20, 21. Geometrites. 1860. 12mo.
— we: Hymenopterous Insects. Part 1. Chalcidide. 1846. 12mo.
Part 2. Additions to Chalcidide. 1848. 12mo.
Catalogue of Hymenopterous Insects. Part 1. Andrenide and Apide.
1853. 12mo. (plates).
——. Part 2. Apide. 1853. 12mo. (plates).
—. Part 35. Mutillide and Pompilide. 1855. 12mo. (plates).
—. Part 4. Sphegide, &. 1856. 12mo. (plates).

Part 5. Vespide. 1857. 12mo. (plates).
Part 6. Formicide. 1858. 12mo. (plates).
Part 7. Dorylide and Thynnide. 1859. 12mo. (plates).
List of Dipterous Insects. Parts] to4. 1848-1849. 12mo.
——. Part 5. Supplement I. 1854. 12mo.
——. Part 6. Supplement II. 1854. 12mo. (woodcuts).
——. Part 7. Supplement III. 1854. 12mo.
Catalogue of Halticide. Part 1. Physapodes and Cidipodes. 1860. 8vo.
List of Homopterous Insects. Part 1. 1850. 12mo.
. Part 2. 1850. 12mo

——. Part3. 1851. 12mo.

—. Part4. 1852. 12mo, (plates),

——. Supplement. 1858. 12mo.

~-— OU Insects. Part 1. 1851. 12mo. (plates).

Part 2. 1852. 12mo. (plates).

Catalogue of Orthopterous Insects. Part 1. Phasmidz. 1859. 4to. (plates).

Nomenclature of Coleopterous Insects. Part 1. Cetoniade. 1847. 12mo.

Part 2. Hydrocanthari. 1847. 12mo.

——. Part 3. Buprestide. 1848. 12mo

—. Part 4. Cleride. 1849. 12mo.

Part 6. Passalide. 1852. 12mo. (plates).

Catalogue of Coleopterous Insects. Part7. Longicornia, I. 1853. 12mo.
(plates).

as Part 8. Longicornia, IT. 1855. 12mo. (plates).

. Part 9. Cassidide. 1856. 12mo.

Catalogue of the Coleopterous Insects of Madeira. 1857. S8vo.

List of the Coleopterous Insects. Part 1. Cucujide, &c. 1851. 12mo.

Catalogue of Hispidee. 1858. 8vo. (plates).

List of Crustacea. 1847. 12mo.

Catalogue of Crustacea. Part 1. Leucosiade. 1855. 12mo.

568 DONATIONS.

Catalogues of the Natural History Collections in the British Museum
(continued),

Catalogue of Myriapoda. Part 1. Chilopoda. 1856. 12mo.

List of Myriapoda. 1844. 12mo.

Sete of Neuropterous Insects. Part 1. Phryganides—Perlides. 1852.
amo. ;

——. Part 2. Sialide—Nemoptrides. 1853. 12mo.

——. Part 3. Termitidx, &. 1853. 12mo.

Part 4. Odonata. 1853. 12mo.

Catalogue of Neuropterous Insects. Part 1. Termitina. 1858. 12mo.

Guide to the Systematic Distribution of the Mollusca. Part 1. 1857. 8vo.

Catalogue of the Collection of Mazatlan Shells. 1857. 12mo.

of Mollusca. Part 1. Cephalopoda Antepedia. 1849. 12mo.

——. Part 2. Pteropoda. 1850. 12mo.

Part 4. Brachiopoda Ancylopoda. 1853. 12mo. (woodcuts).

List of Mollusca. Part 1. Volutide. 1855. 12mo.

Catalogue of Bivalve Mollusca. Part 1. Placentade and Anomiada,
1850. 12mo.

of Conchifera. Part 1. Veneride, Cyprinide, and Glauconomide.
1853. 12mo.

——. Part 2. Petricoladee (concluded), Corbiculade. 1854. 12mo.

Nomenclature of Molluscous Animals and Shells. Part 1. Cyclophoride.
1850. 12mo.

List of Mollusca and Shells, collected, &c., by MM. Eydoux and Souleyet.
1855. 12mo.

List of Shells of the Canaries. 1854. 12mo,

of Cuba. 1854. 12mo.

of South America. 1854. 12mo.

Catalogue of Phaneropneumona. 1852. 12mo.

of Pulmonata. Part 1. 1855. 12mo. (woodcuts).

—— of Auriculidx, Proserpinidx, and Truncatellide. 1857. 12mo.

of Entozoa. 1853. 12mo. (plates).

ist of British Animals. Part 1. Radiata. 1848. 12mo.

Part 2. Sponges. 1848. 12mo.

Part 3. Birds. 1850. 12mo.

Part 4. Crustacea. 1850. 12mo.

Part 5. Lepidoptera. 1856. 12mo.

Part 6. Hymenoptera Aculeata. 1851. 12mo.

Part 7. Mollusca Acephala, and Brachiopoda. 1851. 12mo.

Part 8. Fish. 1851. 12mo.

Part 9. Eggs of British Birds. 1852. 12mo.

Part 10. Lepidoptera (continued). 1852. 12mo.

Part 11. Anoplura. 1853. 12mo.

Part 12. Lepidoptera (continued). 1852. 12mo.

Part 13. Nomenclature of Hymenoptera. 1853. 12mo.

Part 14. Nomenclature of Neuroptera. 1853. 12mo.

Part 15. Nomenclature of Diptera, I. 1853. 12mo.

Part 16. Lepidoptera (completed). 1854. 12mo.

. Part 17. Nomenclature of Anoplura, &c. 1855. 12mo.

Catalogue of British Hymenoptera. Part 1. Apide. 1855. 12mo. (plates).

of Fossorial Hymenoptera, Formicide and Vespide. 1858. 12mo.
(plates).

——. Ichneumonide. 1856. 12mo.

List of British Curculionide. 1856. 12mo.

Catalogue of Recent Echinida. Part 1. Echinida Trregularia. 1855.
12mo. (plates).

Marine Polyzoa. Part 1. Cheilostomata (part). 1852. 12mo. (plates).

——. Part 2. Cheilostomata (part). 1854. 12mo. (plates).

List of British Diatomacer. 1859. 12mo.

3

eee) Peele

DONATIONS. 569

Dawson, J. W. Notes on the Geology of Murray Bay, Lower St.
Lawrence. 1860.

On the Pre-Carboniferous Flora of New Brunswick, Maine,
and Eastern Canada. 1861.

Delesse, A. De Vazote et des maticres organiques dans l’écorce
terrestre. S61. ;

Deshayes, G. P. Analyse du travail de M. Edouard Suess sur les
Brachiopodes de la Collection de Vienne. 1861.

Description des animaux sans vertébres découyerts dans le
bassin de Paris, &c. Livr. 17-22. 1858.

Deslongchamps, EH. Mémoire sur de nombreux ossements de mammi-
feres fossiles de la période géologique dite diluvienne, trouvés aux
environs de Caen. 1861.

Enys, JS. On the jointed Structure of Rocks, as seen from a quarry-
man’s point of view, and its relation to three varieties of cleavage,
viz. slaty, deposit, and granitic. 1859.

Fournet, J. Apercus sur la structure du Jura septentrional. 1861.

Gastald’, B. Frammenti di geologia del Piemonte. Sugli elementi
che compongono i conglomerati mioceni del Piemonte. 1861.

Su alcune ossa di mammiferi fossili del Piemonte. 1860.

Gemmellaro, C. Ulteriori considerazioni sul basalto: appendice
alla vuleanologia dell’ Etna. 1860.

Gras, A. le. Position de quelques écueils dans la mer de corail.
1860. From the Dépot de la Marine.

Renseignements Hydrographiques sur les iles Bashee, les iles
Formose et Lou-Tchou, la Corée, la mer du Japon, et la mer
@Okhotsh. 1860. From the Dépot de la Marine.

Hall, J. Descriptions of New Species of Crinoidea, from investi-
gations of the Iowa Geological Survey. 1861.

Hébert, H. Du terrain jurassique supérieur sur les cétes de la
Manche. 1860.

. Notice sur les Annales de la Société d’Agriculture, Sciences,
Arts et Commerce du Puy. Tome xx., 1855-56. 1860.

Note sur les Trigonies clavellées de ?Oxford-clay et du Coral-
rag. Suivie de la description des fossiles du corallien supérieur
de Glos, par le Dr. Littel et Em. Goubert. 1861.

. Note sur le trayertin de Champigny et sur les couches entre
lesquelles il est compris. 1860.

Quelques remarques sur la mer jurassique et les théories
imaginées pour rendre compte de ses déplacements. 1861.

570 DONATIONS.

Hébert, E. Réponse a la note de M. Ch. d’Orbigny, intitulée: <“‘ Sur
Page véritable des poudingues de Nemours et des sables coquilliers
d@Ormoy.” 1860.

Helloco, C. de. Instructions nautiques sur les traversées d’aller et
de retour de la Manche a Java. 1861. From the Dépét de la
Marie.

Helmersen, G.v. Die geologische Beschaffenheit des untern Naro-
vathals und die Versandung der Naroyvamtndung. 1860.

. Die in Angriff genommenen Steinkohlenlager des Gouverne-
ments Tula. 1860.

Henwood, W.J. Notes on the Silver produced in Cornwall. 1861.

Horsburgh, J. Instructions nautiques sur les mers de ’Inde. Tra-
duites de l’anglais en 1857, par M. le Prédour. 3° édit. Tome
troisieme (2° partie). 1860. From the Dépot de la Marine.

Keller. Notice sur la carte des environs de Cherbourg. 1861.
From the Dépot de la Marine.

Kéralio, de. Histoire naturelle des glaciers de Suisse. Traduction
libre de ’allemand de M.Grouner. 1770. From Prof. J. Tennant,

Longman, W. Suggestions for the Exploration of Iceland. 1861.

Lyons. Résumé des observations recueillées en 1860, dans le bassin
de la Saéne, par les soins de la Commission Hydrométrique de
Lyon, 17° année. 1860. From the Hydrometrical Commission
of Lyons.

Mer du Nord. 3° Partie. Cotes est d’Angleterre. Traduction par
A. le Gras. 1860. From the Dépét de la Marine.

Montigny, C. Sur des débris d’animaux fossiles trouvés prés de
Nivelles. Lettre a M. A. Quetelet. 1860.

Mortillet, G. de. Carte des anciens glaciers du versant italien des
Alpes. 1860.

Newberry, J. S. The Rock-oils of Ohio. 1859,

Oppel, A. Ueber die weissen und rothen Kalke yon Vils im Tyrol.
1861,

Ordway, A. On the supposed identity of the Paradowides Harlan
(Green), with the Paradowides spinosus (Boeck). 1861.

Papers relative to the Exploration by Captain Palliser of that portion
of British North America which lies between the Northern Branch
of the River Saskatchewan and the Frontier of the United States,
and between the Red River and Rocky Mountains. 1859, 1860.
From Dr. J. Hector, F.G.S.

DONATIONS. Cael:

Porter, H. The Geology of Peterborough and its Vicinity. 1861.

Prestwich, J. On some new facts in relation to the Section of the
Cliff at Mundesley, Norfolk. 1861.

—. On the Boring through the Chalk at Kentish Town, London.
1855.

. On the Correlation of the Eocene Tertiaries of England,
France, and Belgium. 1857.

On the Occurrence of Flint-implements associated with the
remains of animals of extinct species in beds of a late geological
period, in France at Amiens, and in England at Hoxne. 1861.

On the Presence of the London Clay in Norfolk as proved by
a Well-boring at Yarmouth. 1860.

Quetelet, A. Observations des Phénoménes Périodiques. 1860.

——. Phénoménes Périodiques: Magnétisme, Astronomie. 1860.

Sur le Congrés International de Statistique tenu 4 Londres
le 16 Juillet, 1860, et les cing jours suivants. 1860.

——. Sur les Phénoménes Périodiques des Plantes et des Animaux.

Rapport sur la partie géologique et minéralogique du voyage de
MM. Grandidier freres (Ernest et Alfred) dans ? Amérique méri-
dionale. Paris, 1860. From M. Hébert.

Report. Fourth Report of the Commissioners for the Exhibition of
1851. 1861. From the Commissioners.

Reinéke. Description hydrographique des cétes septentrionales de
la Russe. 1” partie. Mer Blanche. 1860. rom the Dépot de
la Marine.

Reichel, C. F. Die Basalte und§ siiuleformigen Sandsteine der
Zittauer Gegend in Sachsen und Bohmen. 1852. Presented by
L. Horner, Esq., Pres.Gs.

Roche-Poncie, de la. Note sur l’évaluation des distances en mer,
1860. From the Dépéot de la Marine.

Rogers, H. D, On the Origin of the Parallel Roads of Lochaber
(Glen Roy), Scotland. 1861.

Stoppan, A. Essai sur les conditions générales des couches 4
Avicula contorta. 1861.

Studer, B. Les couches en forme de © dans des Alpes. 1861.

Vallon, A. Influence des courants sur la navigation 4 la céte occi-
dentale d'Afrique. 1860. From the Dépot de la Marine.

THE

QUARTERLY JOURNAL

GEOLOGICAL SOCIETY OF LONDON.

EDITED BY

THE ASSISTANT-SECRETARY OF THE GEOLOGICAL SOCIETY.

VOLUME THE SEVENTEENTH.

1861.

PART Il. MISCELLANEOUS.

CONTENTS OF PART IL.

Alphabetically arranged—the Names of the Authors in capital letters.

Page
Alps (Savoy), A. Favre on the Succession of Beds in the ........ 16
——, Cu. Lory on the Succession of Beds in the.............00. 27
——, 8. Gras on the Succession of Beds in the.................5. 16
Antiporr and Mn@uitzky. Geological Map of the Southern Urals 22
Austria, E. Svrss on the large Tertiary Carnivora of .......... eal
Bayaria (South), F. von Haver on the Molasse af Eases reel eloiscu tres 24
Belgium and North of France, J. GossrLEer on the Paleozoic Rocks
OMe Yee seach rales ssilnne! ie sctydadavenorareualiebenayave: pi suelo suectepal elmett ora] eMart 27
Bohemia, A. E. Reuss on Fossil Freshwater Shells from....... Garetilel
ESKOil= COA), oe OK ORIN VOD vere sven o/s auetey ols lerondl cus seen nepes oasis wvatecsvaretes ouett 6
Bureav on the Existence of Three Divisions in the Devonian Rocks
Grebe NO WeT EOIN Cs cite ay/eiesichelsse te eye evs) ustiebotcnerolatey eioeiiapal ole cease) e ctsike 15
Carnivora, EK. Surss on the large Tertiary................. donot 26
Detesse, A. Geological underground Map of Paris............. 20
—. Hydrological Map of Pape ed ce re sO) Nae aaa 22
——, Studies on the Metamorphism of Rocks................4. 18
Devonian Rocks of the Lower Loire, BuREAU on the ............ 16
Favre, A., on the Liassic and Keuperian Formations of Savoy . 17
ForTTERLE on the Geology of Western) Galicia jw mnyan ire eres ie 7
GCalltctanONWesterm) Geology Ob if vein vsyctaspey) us savas Any <yavaials saison 7
Ceclonicril Mei) OF leh oo oduobdcdaebooodb bode dane o hooadowan - 20
of the South Ural Mountains .....-..--s--s..s0. 00... 22
Ccolocyaok south-eastern Eungary Omnceietscisisas> sees one 11
Git VIG eras EG Eieminnin siento be 46 0 > bro MADR a ao OGG & a
GossELET, J., on the Paleozoic Rocks of Belgium and the North of
HEICAET COU scereacc tc euehsricle to petes dace ein em chen SReA OMAR PALA oper IMB PeNe ctl tic ater 27
GRAS, S., on the Succession of Beds in the Alps.............055 AG
HarpinGer, W., on Meteoric Iron from Nebraska............ peu an)
on Piddingtonite, and a Meteorite from India............... 8
and K. von Haver on the Hauyne-rock of Transylvania .... 30
Haver, F. von, on the Liassic Flora of Transylvania ............ 10
—— on the Molasse of Southern Bavaria ..............cc00000> ne 24,
ou the Mountains South of Kronstadt, Transylvania. ....... 25
Haver, K. von, and W. HarmpIncEr on the Hauyne-rock of Tran-
SINGIN, ConogoooadnscoovenwonoaebopooosonoooOO DO GOOD poncg el)
Ela uyaie-cocks ofebransylyenilaya, sbisrs\oisis ele eee a) apaleisieonoter thei slekercieria ce © 30
Hungary (S.E.), Peters on the Geology of............0.5.. poo | duh
on the Metalliferous Deposits in .................... 12

Hydrological Map of Paris...,. isoovergunn ep doooo Pion oye 508s 22

iv

Page
India, W. Harp1negeEr on a Meteorite from..................-4. :
Jorullo, H. DE SAUSSURE on; the Volcanolof . 0... 4. e eee 138
Kronstadt, F. von Haver on the Mountains 8. of............... 25
Liassic Flora of Transylvania, F. von Haver onthe ............ 10
Lory, Cu., on the Stratigraphical Succession of the Beds in the
Savoy Alps. ret Rea in ee IIR DINE EU ACM RG dG 0 agc-a6 8000 27
Lower Loire, Burau on the Devonian Rocks of the............. 15
Mammalian Fauns of the Vienna Basin, E. Surss on the ........ 1
Meeuitrzky and AntTIpoFF. Geological Map of the Southern Re
fonvot the Ural Mountams erie ie ike kee eke : , 22
Metalliferous Deposits of S.H. Hungary ..............s ss eeeeaee 12
Metamorphism of Rocks, A. DELESSE on the .................44. 18
Meteoric Iron from Nebraska, WHAT INGER Onna none Petrie (9)
Meteorite from India, W. HIAIDINGER: on) a. ). 250.15 eee 8
Molagse’ of Southam ‘Bayaria...:.../. 0c... s,s.) 4. 2. 24.
Nebraska, Meteorite Tron from iiss sje ens alates heioio ous et teenie 9
Paleozoic Rocks of Belgium and North of France......... ioe 27
Paris, A. DELESSE’s Geological EO MIRON EiGmiaa Bins oa0 65 4 > 6 20
Hydrological Map OL Wiis iincee Blais siete Sag ere eee 22
Peat and Brown- coal, PORKOBNY OD 5 i509 'a se sisfscintveke ae ke ee 6
PETERS on the Geology of South-eastern Hungary...........+0.. lel
on the Metalliferous Deposits in S.E. Hungary.............. 12
Piddinetonites; W . EUATDINGER) OD) 0 cape ela. 9: olen aiallan ete 8
PoKoRny on Peat and Brown-coal estes side soe essere 6
Reuss, A. E., on the Fossil Shells of the Freshwater Tertiaries of
13/0] {ost ee ee ep OE AO Dm rtcornon oo oc nor Vat
SaussurrE, H. pr, on the Formation of the Volcano of Jorullo,
IMP ORICON sie vsieee sais vclicig e's ety esac p's veie tee ase. phan oredr cehekalls ON Rag eee 13
Savoy, A. Favre on the Liassic and Keuperian Rocks of ......... 17
, Cu. Lory on the Succession of Beds in..............+--%- 27
, §. GRAS on the Succession of Beds in..|....,:... «ass 16
SonkLAR on the Accumulation of Detritus in the Steinfeld........ 30
Susss, E., on the large Tertiary Carnivora of Austria ............ 26
on the Succession of Mammalian Faunze in the Vienna Basin . i
Transylvania, F. von Haver on the Liassic Flora of ............ 10
: onthe Mountams S> of Kronstadt. sss « 10) eee 25
——, W. HarpineGer and K. von Haver on the ones rock of .. 30
Ural Mountains, Geological Map of the South part of the.......... 22
Vienna Basin, E. Surss on the Mammalian Faune ofthe ........ 1

Volcano of Jorullo, Mexico, H. pk SaussurRE on the .........+-. 13

TRANSLATIONS AND NOTICES
OF

GEOLOGICAL MEMOIRS.

On the Successton of the Mammattan Faunz in the Tertiary Basin
of Vienna. By Prof. EK. Suzss.

[Proceed. Imp. Acad. Vienna, vol. xxxix. 1860, p. 151, &e.]

Tue later Tertiaries of the Vienna Basin have experienced so few
considerable disturbances that a geologist may easily trace the chief
strata filling up this basin, as they follow its margin in concentric
zones, with scarcely any interruption. Marine deposits, dipping from
every side of the extreme margin beneath the more recent central
deposits, are those of most ancient date, although they generally
crop out on the highest points of absolute level. These strata in-
clude innumerable remains of Mollusca, Crustacea, Zoophyta, and
Foraminifera, described by MM. D’Orbigny, Reuss, and Hornes, and
imbedded in layers of sand, rolled pebbles, limestone, marls, or
plastic clay. Great local variety, both in petrographical and palzon-
tological respect, is conspicuous in these strata, although special
researches, continued through years, prove beyond doubt that nearly
all of them (Sands of Neudorf, Leitha-limestone of Steinabrunn,
‘Tegel’ of Baden and Voslau, &c.) have been contemporaneously
deposited on the bottom of one and the same sea,—their differences
not being more striking than those at present occurring in different
sea-zones ; for instance, of the Mediterranean.

The littoral zone ascends the slope of the hills, marking the an-
cient shores, to a level of 1300 feet. At this time, the Vienna region
had its greatest depth beneath the level of the sea; and, in con-
sequence, the communication between the Tertiary seas of Kurope
was more open than at any other period: no wonder, therefore, that
under favourable climatal circumstances so many species could
wander thither from their distant habitats. The occurrence there of
forms bearing a Mediterranean or Indian type is a well-known fact.
Dr. Hornes, in his splendid work on the fossil Mollusca of the
Vienna basin, also describes species reminding us of those at present
living in the West-African seas, such as Cyprea sanguinolenta, Buc-
cmum lyratum, Oliva flammulata, &e.

M. Laurent, in his report on the boring of Artesian Wells in the
VOL, XVII.—PART II, B

2 GEOLOGICAL MEMOIRS.

Sahara*, has remarked, that the portion of this desert lying to the
south of the French possessions bears decidedly the character of an
ancient gulf, formerly connected with the Mediterranean, in the
environs of Gabés. Littoral terraces (the last and most conspicuous
of them called “ Coudiat el Dohor ”) exhibit a continuous series of
“ Falaises,” nearly parallel to the original northern outlines of the
basin, indicating the successive level of the waters and their gra-
dual diminution. Cardiwm edule, imbedded in sand identical with
the sand on the present Mediterranean shores, abounds on the sur-
face in certain places, apparently indicative of shore-lines recently
laid dry; the retreat of the waters having proceeded from the West-
ern Sahara (500-600 metres above the present sea-level) to the east-
ern portion of the desert (now 86 metres beneath this level in the
Schott Melr’ir). Several naturalists have observed Cardium edule
still living in ponds within the desert, and Cyprea Moneta had been
asserted to have been taken in the upper course of the Niger?. A
wide plain south of the Aures Mountains is covered with deposits
characterized as littoral by the presence of Cardiwm edule and an
abundance of rolled pebbles. This occurs in a desert, the level of
which is not unfrequently lower than that of the nearest sea. M.
Buyryt gives to the Melr’ir a higher level than M. Laurent does,
and indicates the Sehott-es-Selam, to the east of it, as the maximum
of depression (—85 metres); atthe same time mentioning the occur-
rence between El Faid and the Oasis Mraie’r of depressions of —41,
—76, —35, —28, and —20 metres; the ground rising again south-
ward in the direction of Tuggurt.

The facts stated by Caillié, and the lately published results of
M. Panet’s § explorations, make it probable that analogous traces of
comparatively recent marine formation may be followed as far as the
Atlantic coast. No hypsometrical measurements of these regions are
known at present; the constitution of the desert, however, and the
local impregnation of its soil with sea-salt may give some indica-
tions in this respect. M. Panet speaks of organic remains and ac-
cumulations of broken shells between alternating layers of salt and
red clay as occurring in the “ Great Sebcha,” an extensive region
abounding in salt and spreading to the 8.W. along the western slope
of the Idjil Range in the district of Aderer. It is to be hoped that
enterprising travellers may soon procure us a more detailed know-
ledge of the traces of this line of communication, so important for
the study of geological geography, as joining the present Mediterra-
nean exactly south of the point where the submarine ridge, running
from south-western Sicily to Tunis, manifests conspicuously its in-
fluence on the distribution of marine animals.

It is a fact worth attention, that extensive sea-shores, rising very
slowly, are generally covered exclusively with sand, rolled pebbles,

* Bulletin de la Société Géologique de France, 1857, vol. xiv. p. 615. ‘
+ See Aucapitaine in Guérin-Méneville’s Revue et Magasin de Zoologie, 1859,
or -

p. 237.
t See Zeitschrift fir d. allzemeine Erdkunde, 1858, iv. p. 298.
§ Petermann’s Geograph. Mittheilungen, 1859, p. 101.

SUESS-—VIENNA BASIN, 3

and remains of strictly littoral shells. An instance of this fact, on
nearly as large a scale, is offered by the great terraced plains de-
seribed by Darwin* as extending from the Rio Colorado to Magel-
hien’s Straits, and overstrewed with sand, rolled pebbles, and re-
mains of shells identical with littoral species of the present age.

This first period of a communication opened to a marine fauna of
prevailing southern (especially Mediterranean) character was fol-
lowed by an upheayal (proceeding chiefly from west to east), and,
consequently, a restriction of the water-surface. Prior to this up-
heaval, a line of Jurassic shoals (girded and partly overlain by
reefs of Nullipore), commencing near the northern margin of the
great fault which cuts the outer secondary zones of the Alps near
Vienna, ran 8.W. to N.E. nearly through the middle of the Tertiary
sea at this time occupying the basin: subsequently the whole grea
west of these shoals was laid dry. The water-surface of the Vienna
basin was then reduced to about half of its former extent, its highest
level not generally rising above 800 feet. This is the epoch of the
Cerithian strata.

The paleontological independence of these deposits, as stated by
Dr. Hornes, is a fact of the highest importance for the true know-
‘ledge of the Vienna basin. Cephalopods, Brachiopods, Bryozoans,
Crustaceans, Echinoderms, and Corals have totally, and Foraminifers
almost totally, disappeared in these strata. The marine fauna is
notably diminished in consequence of the broken communications
with southern seas; and it bears a decidedly Kast-Kuropean cha-
racter. This same fauna continued to coexist in Hungary with the
trachytic eruptions.

Another general upheaval further limited the extent of the water-
area, and was followed by brackish and freshwater deposits with
Melanopsis, Cardium, and Congeria. The basin being now nearly
completely isolated, the fauna became quite different from the pre-
ceding one, and the level of the deposits was again lowered. The
Tertiaries immediately following these “‘ Congerian Strata” are of
fluviatile origin.

It may be considered as a fact beyond all doubt, that during this
period the aquatic fauna-of the Vienna basin underwent several con-
secutive isolations, considerable enough to have repeatedly caused the
extinction of genera and species. Having been persuaded of this
some years ago, I began to follow the traces of the terrestrial animals
known to occur in these groups of strata, as I supposed them to be
altered by climatal circumstances or by the occlusion and re-opening
of communication with other zoological provinces. M. H. von Meyer's
well-known researches on the fossil Mammalia from the environs of
Vienna have been the bases of my investigation. My honoured friend
Prof. C. von Ettingshausen has kindly completed them, by reviewing
his researches on the Tertiary Flora of Vienna, and by tracing the
distinctive characters of several local florse within this region.

The remains of the first terrestrial fauna here must be sought for

* Journal of Researches, &e., pp. 201-207: ‘¢ On South America,” chaps. i. ii.

t For instance, near Ernstbriimn, Staats, Falkenstein, and the hills near Pohlau.
B2

4 - GEOLOGICAL MEMOIRS,

in the marine deposits, especially within the Nullipore-banks of the
oldest tertiary coasts. Undoubtedly many of the large Herbivora of
this epoch may (after they had perished) have been carried by the
water into the then existing bays, and buried there amid littoral
deposits. They are found upon the shores of islets (Leitha Mountains
and Central Moravia), certainly of too limited an extent for the
existence of such colossal creatures. A Dinotherium, an extremely
rare species of Mastodon (of the family Trilophodontes), a large Rhi-
noceros (similar to the Rh. megarhinus of Montpellier, but probably
of a distinct species), Listriodon splendens, H. v. M., a smaller car-
nivorous animal (of the family Canide), the very doubtful Psepho-
phorus, and a small species of Cervus may have existed at this time,
especially on the continent west of the bay. Helix turonica lived on
the sea-shore, especially near Grund. The freshwater shells locally
transported amidst marine deposits are different from those of a
subsequent period. The terrestrial vegetation of this period, as known
at present, consists of remains of drifted wood (Fegonium, Thujoxylon,
Peuce, and Haveria*), and of the strobili of Pinites Partschi (Ktt.),
imbedded in layers in the Leitha-limestone of Mauer, near Vienna.
The fauna just described corresponds, as I have previously remarked’,
to the fauna of Simorre in France, characterized by Listriodon splen-
dens and the Mastodon (if identical in species).

The Cerithian strata, although laid open by extensive quarries, have,
as far as I know, never shown the least trace of terrestrial Mamma-
lian remains, neither in their arenaceous nor in their calcareous or
argillaceous strata. The blue “Tegel” of Hernals and Nussdorf,
lately described by me as a deposit formed at a river’s mouth#, con-
tains yery complete remains of Seals and Dolphins, fluviatile and
paludine Turtles, together with marine Fishes and plenty of land-
plants; but, notwithstanding researches continued through years, I
never succeeded in tracing in them the evidence of any terrestrial
animal. The flora of Hernals, considered by Prof. C. von Ettings-
hausen to be “nearly related to the flora of Parschlug and Tokaj,
and therefore of decidedly Miocene character,’ comprises, among
other forms, a Protacea, a Lawrinea, and a new species of Araucaria.
Recent investigations in the neighbourhood of Lauretta, Purboch, and
Breitenbrunn have, however, shown that the marine marginal deposits
of this district can scarcely be separated from those of the Cerithian
period; the two are in many instances exposed in the same quarry.
Possibly some few of the terrestrial animals enumerated above among
those of the “first fauna”? may rather belong to the Cerithian
period.

The Congerian strata (“ Tegel” of Inzersdorf) provide abundant
facts for the study of the contemporaneous terrestrial fauna, charac-

* Unger, Trans. Imp. Acad. Vienna, vol. xiv.; Beitrage zur nahern Kenntniss
des Leithakalkes.

+ Imp. Geol. Inst. Vienna Annals, in the “Reports of Meetings” for 1858
and 1859.

t Vienna Acad. Proc. vol. xxxvii. p.673 ; Steindachner, “ Beitrage zur Kenntniss
d. foss. Fische Oesterr,”

SUESS—VIENNA BASIN. 5

terized by Dinotherium giganteum, Mastodon longirostris, Rhinoceros
Schleiermacheri, Acerotherium incisivum, and Hippotherium gracile ;
in short, nearly all the species known to constitute the fauna of Kp-
pelsheim. Acerotherium incisiwum and Hippotherium gracile seem to
have numerically prevailed. Not one species is identical with any of
the “‘ marine group,” only the Dinothervum is still subject to some
doubts in this respect. ‘This is the ‘second fauna” of terrestrial
Mammalia. The contemporaneous flora is, according to Prof. C. von
Ettingshausen, richer in species than any other in the Vienna basin.
Thirty of these species have been described*. The whole flora re-
minds one of that of Bilin; and is somewhat posterior in age to that
of Parschlug.

The “Tegel” with Congeria and Melanopsis is locally over-
lain by beds of white quartz-pebbles with external rust-coloured
tinge, imbedding here and there layers of fine sand. This deposit
(“ Belvedere Gravel”) is of fluviatile origin. The whole of the Mam-
mals in the “ Tegel” of Inzersdorf appear again in it, together with
Sus paleocherus, known to occur at Kppelsheim. The nature of the
strata was less favourable to the preservation of the terrestrial flora
than the clay; silicified stems, however, of Conifer, and fruits and
peduncles of a Steinhauera (Ktt.), are not of rare occurrence. A
Valvata and a Helix are the only mollusca known at present to occur
in these gravels. Notwithstanding the petrographical differences,
the mammalian fauna of the “ Belvedere Gravels” and the lacustrine
plastic clay of Inzersdorf remained identical. The lacustrine molluscan
fauna alone became extinct. The flora does not offer sufficient ma~
terials for comparison.

The deposits just mentioned are overlain, to my knowledge, by
two fossiliferous strata of doubtful contemporaneity, merely local and
restricted in their extent. The first of them is a clay, found by M.
Kapper, at the Eichkogel, near Modling (8. of Vienna)?. It con-
tains vegetable remains, which have been referred by Prof. C. von
Kttingshausen to the youngest tertiary flora, characterized by the
presence of Saliv angusta, Glyptostrobus Oeningensis, and Juglans
latifolia ; possessing these species in common with the flora of Oenin-
gen in Bavaria.

The other of these deposits is a bed of fluviatile rolled pebbles,
differing from those of the ‘‘ Belvedere Gravel” by being less in size
and derived from divers Alpine rocks. No remains of the “Second
Mammalian Fauna” have occurred among them. In one case they
have been found to include a molar different from that of Elephas
primgenius (probably of Hl. meridionalis). To these strata may
likewise belong a tooth of Hippopotamus, preserved in the Imperial
Museum of Vienna, and hitherto the only remains of this genus known
to have been found within the Vienna basin. These remains may
be indicative of a “Third Mammalian Fauna” possibly analogous to
that which has recently been called “ Pliocene Fauna” (Val d’ Arno).
As far as I know, this stratum has been stated to occur only within

* Ettingshausen, in Vienna Geol. Inst. Trans., ‘‘ Die fossile Flora yon Wien.”
t+ Annals of the Vienna Geol. Inst. 1859, p. 25.

6 GEOLOGICAL MEMOIRS.

the immediate vicinity of Vienna itself, in the suburbs of Landstrasse
and Reinprechtsdorf; nor can its paleeontological independence be
asserted yet with certainty.

The uppermost deposit is loam (Loess), with subordinate and oc-
casionally considerable layers of fluviatile rolled pebbles. In this we
find the representatives of the “‘ Fourth Mammalian Fauna ” (Hlephas
prumgenius, Rhinoceros tichorhinus, Ursus speleus, Hyena spelea,&e.).
Analogous as the molluscan fauna of this loam is to that of the pre-
sent times, certain species (Helix pomatia, H. Austriaca, H. verti-
clus, and H. ericetorum) are absolutely wanting in it; and by this
negative character the “ Loess” may be conveniently distinguished
from the loam of less ancient date, frequently covering the lowest
portion of our valleys. This “‘ Fourth Fauna” is generally considered
to be post-tertiary. Before its appearance a small portion of the
Vienna basin had been again invaded by sea-water; and perhaps our
present mammalian fauna may hold the fifth place in the whole series.

It is a fact that several hundreds of the marine species of the
Vienna basin coeval with the “ First Mammalian Fauna” are still
existing, chiefly in the Mediterranean, while the mammalian fauna
has undergone three or four changes.

The more I recall to memory these chief results of several years’
investigations, the more I see how each group of terrestrial or aquatic
animals is imbedded in strata different in petrographical character, in
extension, and in level, every one keeping up its independence, while
the terrestrial mammals offer in some degree representatives of the
precedent and subsequent faune. The more I attend to change of
coast-line, the transition of marine to brackish, lacustrine, and finally
fluviatile deposits, and the changes in the course of rivers, manifested
by the diversity of the gravels, the less I feel the necessity of adopt-
ing an hypothesis as bold as is that of a “ Species-life ” (Artleben).
The repeated extinction of these organized bemgs appears to me
rather as a necessary consequence of the change of external condi-
tions, as they may be traced in the present case. Within the Vienna
basin, communication has prevailed with respect to terrestrial animals,
and solation as far as aquatic animals were concerned.

The terrestrial flora has equally undergone more than one change ;
and possibly the repeated extinction of mammals may have been a
merely secondary fact, connected with these changes of vegetation.

Among others, the fossil fauna of Pikermi, near Athens, entitles
us to suppose that at least one or the other of the above-mentioned
mammalian faune was not spread uniformly over the whole surface
of Europe, as it exists at the present time. [E. 8.]

On Prat and Brown-coat. By Professor Poxorny.
[Proceed. Imp. Geol. Instit. Vienna, April 17, 1860.]

Pror. Poxorny has lately visited the principal Peat-bogs of the
Austrian Empire, and published the results obtained by him in the
‘ Transactions’ of the Vienna Zoologico-Botanical Society, in whose

FOETTERLE—-WESTERN GALICIA. 7

Museum he deposited a collection of 130 specimens of Peat. The
varieties of this substance may be distributed into four groups :—
(1.) Vegetables in progress towards their conversion into peat;
(2.) Peat in its proper sense; (3.) Carboniferous resinous substances ;
(4.) Half-peats. To the first group belong the isolated patches of
Carex stricta, rising above the level of the surrounding moors, and
which in Hungary are known under the name of “ Zsombek,” the
thin layers of peat covered with moss, grass, or rushes, and the
fragments of wood included in peat. ‘To the second group belong
the moors of the plains overlying inorganic strata, and impregnated
with earthy and saline particles by the waters irrigating them, and
the mountain-moors, or high moors overlying—sometimes at a con-
siderable depth—the detritus of forest-, heath-, or moor-vegetation,
and irrigated by water free from inorganic substances. The plain-
or rush-moors produce brown, fibrous, or amorphons peat, of dry
consistence, and, on their surface, a variety (meadow- or pitch-turf)
of darker colour and more compact structure, but more mixed with
other substances. The peat of mowntain-moors is purer; its specific
weight (not compressed) varies between 0°5 and 0:8; and it is espe-
cially adapted for the heating of boilers and for metallurgical pur-
poses. An earthy variety from Zips (N. Hungary) bears great re-
semblance to the “‘ Umbra” of Cologne. The “ Dopplerite”’ of Aussee
(Styria) and analogous substances from the peat-bogs of Switzerland
and Berchtesgaden, described by MM. Deicke and Giimbel, consti-
tute the third group. ‘The half-peats (fourth group) are mixed with
notable proportions of inorganic substances, and, although capable
of slow combustion, cannot be ranked among peats if this portion
amounts to 30-50 per cent. [Counr M.]

On the GEoLoey of Wrstern Ganicra. By M. Forrrerte.
[ Proceed. Imp. Geol. Instit. Vienna, April 24, 1860.]

Lower Secondary deposits, connected on the W. and HK. with those
of Hungary (Red Sandstone, Triassic Dolomite, Kossen and Adneth
strata), appear only on the northern slope of the Tatra mountain-
group, resting on granite and partly overlain by Nummulitic lime-
store and menilite-slate. A powerful range of Triassic limestone
runs northward of the Carpathians from Rozagnik to Innwald,
stretching H. and W. into Hungary; it is associated with Liassic
and Neocomian marls.

The Neocomian beds (Hoheneger’s “ Teschen Slates’) extend W.
and EK. from Biala (Silesia) to Tarnow (Galicia), and 8. of Biala in
the same degree of development. The Carpathian Sandstone pre-
vails within the region in question. The lowermost, non-fossili-
ferous, strata are Cretaceous. A Fucoid with a spiral axis, like
Fucoides Brianteus, and common to the Gosau-marls and to the Fu-
coid-marls near Vienna, occurs in this sandstone near Neumarkt.

The upper Nummulitic (consequently Kocene) strata of the Car-
pathian Sandstone are far spread about Saypath, Tordanow, between
Neumarkt and the Tatra; they are overlain by a thick mass of

8 GEOLOGICAL MEMOIRS.

sandstones, alternating in their basal portion with black slates, con-
taining (like the menilite-slates of the uppermost Hocene) fragments
of Lepidopides leptospondylus, Heck., Meletta longimana, Heck., &e.
They occupy the valleys and depressions, and are highly impregnated
with bitumen, which is exploited as naphtha in several localities.
The overlying coarse-grained sandstones, extending south-eastward
to Eastern Galicia and Bukowina, occupy the higher horizons. The
greater portion of the argillaceous iron-ores worked in Eastern
Galicia are connected with the above-mentioned black slates. Upper
Kocene Tertiaries, abundant in salt, gypsum, and sulphur, are con-
fined to a narrow band along the northern extreme edge of the
Tatra, and generally disappear beneath a great deposit of loam
(Liss). Eruptive rocks (trachyte and diorite) appear on a small
scale in some few isolated localities. [Counr M. ]

On Pippinetonire, and a Merrorrte from East Inpra.
By Director W. Harpreer.

[ Proceed. Vienna Imp. Acad. Sciences, June 8, 1860.]

A correction of Indian Meteorites that came into the possession of
the Imperial Museum of Vienna (in June, 1860), by way of exchange,
through the good offices of Messrs. Oldham and Atkinson, contains
specimens from Allahabad (Futteh-poor, Noy. 30th, 1822), Shalka
(Nov. 30th, 1850), Segowlee (March 6th, 1853), Assam (1846,
found by the late Mr. Piddington), Pegu (brought by Mr. Oldham
from Ava), and a fragment of the still problematic lumps of iron,
weighing 156 lbs., found on the Kurrak-poor Hills, near Monghin,
on the banks of the Ganges. The first specimen examined (from
Shalka, 1850) has proved to be nearly entirely composed of a non-
descript mineral substance, which Director Haidinger has named
«‘ Piddinetonite,’’ in honour of the late Mr. Piddington, Curator
of the Calcutta Museum of Practical Geology, known to the scientific
world by his able researches on Cyclones, and to whose exertions we
are indebted for the preservation of the still extant fragments of
this originally very large Meteorite, and for its first scientific inves-
tigation in the ‘Journal of the Asiatic Society of Bengal’ (vol. xx.
1852). Piddingtonite is of ash-grey colour, more or less fine-
grained, very fragile, although of considerable hardness (6:5 Mohs,
or between felspar and quartz), more or less translucid, of oil-like
brightness, imperfectly cleavable in two directions intersecting at
angles of about 80° and 100°, and without magnetie¢ action.

The whole meteorite is of a breccia-like aspect, interspersed with
minute grains and incomplete crystals of black chromate of iron ; its
crust is dark-brown, and nearly opaque. About 9 lbs. weight was
saved for the Calcutta Museum, the rest having been taken by the
people of the surrounding country. ‘The fall, with the usual phe-
nomena of light and detonations, took place three hours before sun-
rise, in a clear starry sky: the stone coming down in a direction
of S. to N., and under an elevation of 80°, penetrated 3 feet deep
into the soft ground of a rice-field. When dug out next morning,

HAIDINGER—-METEORIC IRON. 9

it was quite cool; the surrounding ground, however, had evidently
been altered by the action of heat. The original size could not be
perfectly ascertained ; certainly the breadth and length of the stone
were not less than one foot; its height was probably still more:
fragments were found at 3 feet depth, and others were scattered
on the surface within 20 feet circumference. [Counr M.]

On the Merrortc Iron from Nusraska. By Director W. Harrier.
[Proceed. Vienna Imp. Acad. Sciences, December 13, 1860.]

A FRAGMENT of a specimen of this iron preserved in the Museum of
St. Louis (U.8.), arrived at Vienna (as promised by Mr. Nath.
Holmes, Secretary of the St. Louis Academy) on October 30, 1860,
by the care of the Smithsonian Institution. The fragment, weigh-
ing 1 1b. 4,5, ounces, was cut in two pieces parallel to its longi-
tudinal axis, and the cut faces were polished. One of these pieces,
21 inches in length, 2 inches in breadth, and 10 lines thick where
it is thickest, shows on one side the original surface, nearly even,
with very shallow depressions confined by rounded edges, and with
some trace of the dark-brown crust still preserved in the con-
cavities. The weight of this piece is 8% ounces. The plane of the
cutting shows strings of whitish colour indicative of crystalline’
structure (‘‘ Widmannstetten’s figures”); and, by a lucky chance,

the direction of the eut fell nearly parallel to the plane of an
- octahedron. The “stripes” intersecting, at angles of 60° and 120°,
the triangular and rhombic “intermediate ares” between “ pro-
jecting borders” of Schreibersite are conspicuous over the whole
surface, after having been submitted to the etching-process, and
keep a constant and perfectly parallel disposition. It cannot,
therefore, be doubted that this iron went through a process of
erystallization during a period as yet unmeasurable.

The cleavage or lamellar structure parallel to the planes of the cube,
as it appears on the meteoric iron of Hauptmannsdorf, near Braunau
(July 14, 1847), is not conspicuous on the Nebraska iron ; nor does
the latter show the damask-like crystalline patterns of the irons of
Bohumilitz and Basin. It exhibits rather the genuine “ Widmann-
stetten’s figures,” such as are conspicuous on the meteoric irons of
Elbogam, Agram, and Aurange; coming next in texture to the large
1-635 lb. mass from Red River (Louisiana), or to the iron from
Texas (Vala Colluja) described and autotyped in Silliman’s ‘ Ameri-
can Journal.’ The white zigzag lines, conspicuous in the figure, are
produced by crevices in the crystalline substance, parallel to the
planes of the octahedron. The white round spots indicate the places
where the action of the acid has penetrated to a greater depth around
central particles of sulphuretted iron.

The second piece obtained by cutting is of 10 ounces weight, nearly
4 inches in length, 24 in breadth, and 1 to 4 inch in thickness,

An excellent lithographic figure of the Nebraska iron, in the
‘Transactions’ of the St. Louis Academy, vol. i., shows it from the
side which may be supposed to be that opposite to the direction of

10 _ GEOLOGICAL MEMOIRS,

the meteor during its course through the atmosphere, as it presents
a great number of such shallow depressions as are so conspicuous in
the Meteorite of Gross Divina, which fell July 24, 1837. (See
Haidinger, ‘ Proceedings’ Vienna Academy, vol. xl. 1860, p. 528.)
According to Mr. N. Holmes, the iron in question was found on
the right shore of the Missouri, in the Nebraska Territory, 20 miles
from Fort Pinoon (44° 19’ N. Lat., 100° 26’ W. Long. from Green-
wich), in 1857, by Mr. C. P. Chouteau, who in the spring of the
following year presented it to the Academy of St. Louis. When first
found, its surface was but very little altered by rust.
Mr, A. Prout analysed it, and found
Tron oii. oe) cyan ie reo Omar cents
NIG aE RSIS)
Magnesium: «)55% 5. 650
Calera: scale hes wre teem < *350
Sulphur’. ja We Yer ena Westize

102-473

No trace of cobalt, manganese, chrome, or any other substances
besides the five named above could be made out. Perhaps the
“projecting borders,’ supposed above to be Schreibersite, may
prove upon closer examination to consist of a phosphuret of iron
~and nickel. The specific weight of the whole, at a temperature
of + 12°, is 7:362; it may be supposed to be somewhat higher
in smaller fragments, as superficial crevices seem to indicate the
existence of internal solutions of continuity. [Count M. }

99
39
39

On the Lrasstc Frora of TransytyantA. By Franz von Haver.
[ Proceed. Vienna Imp. Geol. Instit., March 13, 1860.]

A contEction of plants made by Prof. Meschendorfer, of Kronstadt,
from a black slate at Holback and a light-yellow micaceous quartz-
ose sandstone at Neustadt, in the Siebenbiirgen, which are regarded
as equivalent to the “ Gresten Strata” and of Liassic age, consists of
the following species :—

a, From Holback.

Cyclopteris, sp. (?); fragments of a very large species.

Anthopteris meniscoides, Brongn. (Found also near Bayreuth.)

Taniopteris vittata, Brongn.: not well preserved. (Found
also in England.)

Zamites Schmiedeli, Sternb.: badly preserved, but distinct.
(Found also in Franconia and in the Liassic Coal of
Steierdorf.)

Zamites, sp. (or Pterophyllum?); in fragments.

Pterophyllum rigidum, Andr. (Also found at Steierdorf.)

Cunninghamites sphenolepis, Braun. (Found also in Franco-
nia and at Fiinfkirchen in Hungary.)

b. From Neustadt.

Zamites Schmiedeli, Sternb. A large specimen, beautifully

preserved,

REUSS—TERTIARY SHELLS OF BOHEMIA. Ay

Zamites, n. sp. (Also found at Steierdorf and in the Vene-
tian Alps.)
Pterophyllum rigidum, Andr.
This flora may be considered as identical with that of Steierdorf
in Banat, and consequently with that of the Lettenkohle of Bayreuth,
belonging to the horizon of the “ Bone-bed.” [Count M. |

On the Fosstn Suxtts of the Freswater TertiaRies of BonEMIA.
By Prof. A. E. Reuss,

[Proceed. Vienna Imp. Acad. Sciences, June 8, 1860.]

Tuer molluscan species at present known to occur in the freshwater
tertiary limestones of Bohemia amount to 68, distributed as follows :
—Cyclostomacea 1, Aciculacea 2, Helicinea 50, Lamnceacea 12, Cy-
cladida 3. Among the 50 Helicinea there are 24 species of Hela,
3 of Bulimus, 6 of Glandina, 7 of Pupa, and 7 of Clausila. The
prevalence of Clausilie (nearly all of new species) gives a particular
feature to this fauna, as they abound in it more than in any other
locality of analogous nature. Among them, Clausilia vulgata and
Cl. peregrina, Reuss, are already described: the new species (Cl.
tenmsculpta, Cl. denticulata, Cl. polyodon, and Cl. amphiodon) are all
very nearly related to the present European forms. A shell of the
family Limneacea constitutes a new generic type, named “ Acro-
chasma”’ on account of the structure of its shell. The only known
species (Acrochasma tricarinatum, Reuss) has a trilateral pyramidal
shell rounded below in its whole amplitude, with one posterior con-
cave, and two lateral slightly convex planes, ending upwards in an
acute reflected apex, beneath with a longitudinal aperture through the
shell, which in its living state seems to have been covered with an
epidermis. The new genus stands next to Ancylus, and may be con-
sidered as a freshwater representative of the marine genus Fisswrella,
Among the 68 species from the Bohemian freshwater limestones,
15 (or nearly 1th) are identical with those from the analogous deposits
of Hochheim, in the Mayence basin. Eleven other species bear such
a resemblance to some from the same locality that they may be said
to represent them. From these facts it may be concluded that the
Bohemian and the Mayence freshwater limestones were coeval.
[Count M.]

On the Grotoey of Sourn-Eastrrn Huneary. By Prof. Purers,
[| Proceed. Vienna Imp. Acad. Sciences, June 8, 1860. ]

THE mountainous district of Bihdr, well-known for the rich metalli-
ferous veins and the fine mineralogical specimens of Rézbdnya, lies
enclosed between the metalliferous mountains of Banat and N.E.
Hungary, the Transylvanian Highlands, and the great Centro-Hun-
garian plain. Its stratified deposits, save some peculiarities in their
development, are the same as at Banat: its structure and connexion,
as a whole, with its main range, its intervening hills, and its partly
isolated eruptive masses remind one as much of the uniform mica-

12 GEOLOGICAL MEMOIRS.

schist ranges in the Koros, Szimos, and Berettyo valleys, as of the
masses around Nagybinya. ‘The red slates and sandstones (probably
«Old Red”) and the Carboniferous strata immediately overlying the
mica-schists of the Banat are again met with in the Bihdr mountain-
group. The Liassic limestones and sandstones (although non-carbo-
niferous) are well developed and identical with the Alpine ‘“ Gresten
strata.” Triassic strata and those intervening between Trias and Lias
seem to be totally wanting.

Jurassic deposits intimately connected with Neocomian strata are
represented by Carpathian Cliff-limestones and (probably) ‘‘ Klaus
strata.’ The tertiary Congerian clay is of general occurrence as far
as the foot of the high mountains; Cerithian strata nowhere ad-
vancing so far upwards. The Neogene deposits of Bihdr agree exactly
with those of Central Hungary. Among the massive rocks, a strati-
fied euritic porphyry with remarkable tufts, porphyroid rocks of less
remote date, and a particular variety of syenite of relatively very
recent date are conspicuously prevalent. All these rocks have acted
most powerfully in the disturbance of strata and in the distribution
of metalliferous minerals. A large mass of trachyte and an eruptive
rock of the variety named “ Rhyolite’”’ by Baron Richthofen have
been observed. [Count M.]

On the MerattrrErovs Duposits in 8.E. Huneary. By Prof. Pzrers.
[ Proceed. Vienna Imp. Acad. Sciences, July 12, 1860.]

Tur rich deposits of lead- and copper-ores, exploited in the district
of Rézbinya, are not veins, as generally supposed, but massives,
associated with ckastic rocks and intercalated into Jurassic and Neo-
comian strata. The eruptive rocks (syenite and greenstones) con-
nected with them are concerned in the origin of these metalliferous
deposits ; their violent action having caused disruptions, into which
the ores were subsequently deposited. At a certain depth ores are
found together with rocks produced by contact, and mineralogically
analogous to the wollastonite-rock of Banat, and in some sort with
those of Monzoni (8. Tyrol), Mount Vesuvius, &c.

The magnetic iron-ores occur, as in Banat, at the contact of
syenite and Jurassic limestone, and are of great importance, espe-
cially near Potrosz, although still neglected for want of capital.
More than 60 mineral species occur in the mining district of Réz-
binya. Among them, simple and binary compounds of tellurium
with silver, copper, and arsenic, buratite (Delesse), associated with
smithsonite and calcareous spar, linarite and caledonite, connected
with carbonate of lead and galena, brochantite (not stanniferous, as
Prof. Magnus thought it to be), a new hydrosilicate of magnesia,
potash, and alum (erroneously named agalmatolite), and a hydro-
borate of soda and magnesia (very probably isomorphous with the
boro-calcite of Iquique), appearing in the shape of microscopical
acicular groups in a granular limestone modified by contact, deserve
particular attention. [Counr M.]

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Formation of the Voucano of Jorutto, Mexico.

By M. H. pz Saussure, of Geneva.
[Bulletin de la Société Vaudoise des Sciences Naturelles., 1859, No. 45, vol. vi.
pp. 195-197. (Séance du 22 Juin, 1859.)]
Tr is, this very year, precisely a century since the fine valley of
Jorullo witnessed the transformation of its surface, previously covered
with plantations of indigo and sugar-cane, into a barren sheet of
stony lava. This catastrophe had for one of its results a perfectly
characterized volcanic mountain, which suddenly sprung up on the
surface of the globe, with unexampled rapidity and grandeur of pro-
portions.

The importance of this phenomenon in a geological point of view
is great, from the conclusions to which it has been supposed to lead.
Too much attention therefore cannot be given to the study of its
mode of action, especially as the latter has been wrongly interpreted,
and has been applied to support theories of an absolutely unfounded
character.

Humboldt, who visited the volcano only forty-three years after its
first appearance, considered it as the consequence of upheaval (sou-
lévement). According to him, the immense sheet of lava which sur-
rounds the mountain is the result of a softening of the pre-existing
surface-soil (sol) by gases, and its inflation from beneath like a
bladder. The border of this sheet of lava is, according to him, the
broken edge of the kind of table which the subterranean action thus
heaved up. This opinion served as an argument in favour of the
theory of ‘‘ Craters of Elevation” of von Buch, which ascribes to
other volcanos the same origin. But the very first imspection of the
locality suffices to show that such an opinion cannot be sustained in
the present state of the science. In my opinion Jorullo is not the
result of any kind of elevation, but has been produced solely by
means of eruplion and accumulation. The sheets of lava, called
<< Malpais,” are nothing else than vast outflows of incandescent
matter, which have lined the whole valley, filling its cavities and
forming promontories, just as a mass of molten lead would spread
when poured on an uneven surface. The edges of the ‘‘ Malpais,”’
raised from 30 to 80 feet in height, are not a section or broken »
edge of an elevated tract, but only the lateral or terminal borders of
currents of lava. The cone which forms the mountain of Jorullo
itself is the simple result of the heaping up of cinders and scorie
ejected by the principal orifice of eruption.

The volcano of Jorullo, in fact, is composed—
VOL. XVII.—PART II.

14 GEOLOGICAL MEMOIRS.

First, of the sea of lava which resulted from several repeated out-
bursts of lava from fissures, which outbursts, successively lessened in
the area covered by each, as it overflowed the preceding one, formed
four distinct terraces or steps, one higher than the other.

Secondly, of a central cone raised above these lavas after they had
ceased to flow, by the gaseous eruptions.

Thirdly, of one great and last current of lava which flowed from
the summit of the cone and encircled its base. This current was
due to the emission of lava after the gaseous explosions which formed
the cone had terminated.

Lastly, the remnant of lava which remained in the hollow of the
cone, as in a basin, by degrees sank within it as the subterranean
action ceased and the lava-column in the chimney subsided, from
which resulted a series of concentric ruptures and subsidences which
form the vast cavity of the crater.

Besides the principal cone, there is also a series of small cones
arranged on one line, which are only heaps of ejected scorie and
ashes, and do not appear to have produced any lava. Their arrange-
ment shows the eruption to have taken place from an axial fissure
running N.S. But there is no trace of the elevation (sowlévement)
of the beds along this axis, which proves that the volcanic pressure
from beneath had not broken up the surface-beds, but only forced
an exit through some fault in them for the escape of the liquid and
fluid matters erupted.

Other small cones of ashes are scattered about at some distance
from the principal one. It will be seen from what has been said,
that the principal cone rises from a base of lava already high. In
fact, the surface of the “‘ Malpais”’ rapidly rises from its edges to the
foot of the cones. This highest point forms, according to Humboldt,
the summit of the raised ‘“ bladder”’ of lava, and of the “ upheaved ”
plain. I do not think its structure is to be viewed in any such light.
The imperfect drawing of Jorullo published by the illustrious traveller
propagated his error among other geologists. The surface in the
midst of which the volcano broke out, was not a “ plain,” as Hum-
boldt erroneously calls it, but a very uneven valley; nor was it in
the bottom of this that the fissure opened whence issued the basaltic
lavas which covered the neighbouring surfaces, but on the eastern
slopes of the valley, and in a direction parallel to its axis, so that
the great height of their culminating portion is due im part to the
previous height of the surface beneath, and explains itself without
the necessity of supposing any upheaval.

It should be added that the highest portion of the “‘ Malpais” was
still further raised by the superposition of several successive sheets
of lava, which did not reach the outer limits.

It is evident, then, that the voleano of Jorullo has been formed in
no degree by upheaval, and that its phenomena, far from pleading in
favour of the upheaving action of the volcanic force, show, on the
contrary, that the most powerful volcanic outbursts can take place
without the slightest derangement of the superficial beds.

[G. P. S.J

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the Existence of Turen Divistons in the Devontan Rocxs of the
Lower Lorrr. By Dr. Burzav.

[Bulletin de la Société Géologique de France, 2° série, vol. xvii. pp. 789-796. ]
Tue Devonian rocks of the Lower Loire rest on metamorphic slates,
which graduate downwards into mica-schist, finally resting on the
granite of La Vendée. The whole mass is divisible geographically
into a northern development of grits, coal-beds, and conglomerates,
and a southern one of clay-slates with associated limestones.

1. Lower Devonian. These form the southernmost beds, and con-
tain Plewrodictyum problematicum and Leptena depressa. The lime-
stones contain Corals, of which Calamopora Goldfussu is the type.

2. Middle Devonian. Proceeding northwards, a band of slaty
limestone is met with, sometimes pink and in other places black,
characterized by Stringocephalus Burtina.

3. The upper schists are charged with numerous Brachiopods,
described by Dubuisson in 1830. In the same beds Dr. Bureau dis-
covered fragments of Plants. He doubtingly separates these schists
from the Middle Devonian on paleontological evidence. A gradual
change carries this slaty rock into the upper grits, which constitute,
with subordinate coal-beds and conglomerates, the northern expo-
sure of the Devonians. ‘The limestones occurring here are charged
with Terebratula cuboides, T. pugnus, &. The grits and coal-beds
alternate four or five times, in parallel stratification. The flora of
the coal-beds differs from the great Carboniferous flora, although
there are some species common to both. Ferns are represented by
Sphenopteris.

The slates containing Spirifer Vernewli (which the French
geologists always class with Devonian rocks, although our Dublin
neighbours label them as Lower Carboniferous) are entirely absent in
this district.

Dr. Bureau’s expected work on the details of the district will
doubtless aid in the construction of a true Devonian flora, and con-
tribute to the determinate classification of an interesting series of
rocks which at present are occasionally claimed as Carboniferous.

[iss Tie e sy]
D

VOL, XVII.—PART. II.

16 GEOLOGICAL MEMOIRS.

On the Liasstc and Knuprrtan Formations of Savoy.
By AtpHonsE Favre.
[Mémoire sur les Terrains Liasique et Keupérien de la Savoie: par Alphonse
Favre, Professeur de la Géologie 4 Académie de Genéve. (Geneva, 1859, 4to,

pp. 92, with 3 plates.) Extrait du tome xv. des Mémoires de la Société de
Physique et d’ Histoire Naturelle de Genéve. |

On the ContraRiEty observable in the Aups between the STRATIGRAPHICAL
Succusston of the Beps and their PaLmontoLocicaL Contents ; with
an Additional Example of this Contrariety. By Scrpro Gras.
[Considérations sur l’Opposition que l’on observe souvent dans les Alpes entre

Vordre stratigraphique des couches et leurs caractéres paléontologiques, suivies

d’un nouvel exemple de cette opposition. Par M. Scipion Gras, Ingénieur en
chef des Mines. Annales des Mines, 5™¢ sér. vol. xviii. 4° livr. de 1860, pp. 17-54.]

Tue great interest which just now attaches to the study of Alpine
geology arises from its striking exhibition of apparent exceptions to
the established order of superposition.

M. Favre thus states the case :—

“In the Tarentaise, Coal-plants and Oolitic fossils appear to be
associated together. Controversy as to this has lasted for thirty
years, and affects the very foundations of paleontology.

“‘In the valley of Chamouni, Jurassic limestone is seen dipping
beneath crystalline rocks.

“In the valley of Reposoir, rocks containing Ammonites and
Belemnites rest on Nummulitic beds.

“In the hills of Coux and Goléze, Liassic or older rocks rest on
Nummulitic strata.

“At the base of the Mole, the strata are Neocomian by fossils
and Jurassic by position.”

T'wo leading theories have been advanced respecting these and
similar cases. One, which is well represented by M. Favre in the
work referred to, is that they are due to enormous folds and faults ;
the other, advocated by the mining engineer in chief, M. Scipio Gras,
in the second work, that they are actual local exceptions.

M. Favre says, referring to the instances above quoted :—

‘Tn spite of these observations, I neither believe in the contem-
poraneity of Coal and Jurassic fossils, nor in the inferiority of
Ammonite-beds to Nummulitic, nor that the latter are older than
the Lias, still less that the Neocomian were anterior to the Jurassic,
or Tertiary rocks to Secondary.”

A problem of so much interest to geology, when thus clearly stated,
and illustrated by carefully delineated surveys, is well worth atten-
tion. The two publications before us, especially the former with its
admirable sections, furnish ample materials.

M. Favre first describes the rocks of Meillerie and of the Dranse.
They form part of the great Liassic chain stretching from the shore
of the Lake of Geneva to the Arve, from Meillerie to the Mole. They
consist of a quadruple series, which, according to our author, is
folded four times on or, rather, within itself. The lowest group is

FAVRE AND GRAS—ALPS. 107/

the Toarcian,—marly beds with cement-stones; characterized by
Ammonites Aalensis. 2. Liassicand Sinemurian. 3. Kossen beds (Avi-
cula contorta beds). 4. Dolomitic cellular limestone, of large develop-
ment and constant position throughout the Alps, called ‘‘Cargneules.”
The last two are classed with the Keuper; the first two with the
Lower Jurassic or Liassic. The picturesque gorge of the Dranse
exhibits the same series; but the ends of the plications are here
apparent. The 4th group attains great thickness, and contains large
masses of gypsum at Feterne and Epine.

Associated with the latter are bituminous coal and jet. Down-
wards it extends into the representatives of the saliferous red rocks
of the Jura.

M. Favre has a highly interesting chapter on the intermingling
of fossils in these rocks; he makes out numerically that some few
species are common to the Lias and the Trias, and a larger propor-
tion common to more than one stage of the Lias. He then describes
various other localities in which the Kossen beds are surmounted by
Liassic strata, especially at Tanage, where both are underlain by
anthracitic deposits. He then describes extensive sections across
the Trias, Lias, and Jura. Mont Blanc is enveloped in Keuper
rocks (Marnes irisées); and although the discovery of instructive
sections was as difficult to him as to Mr. Ruskin, yet he con-
cludes—* The beds are here found in an inverted order of super-
position. This fact, so long doubted, appears to me to be completely
proved by the relative position of the gypsum-beds and the Triassic
‘ cargneules.’ ”

He next dwells on the correlation of the Lias of Savoy with
formations of the same age elsewhere, and on the extent of their
metamorphism.

We now turn from this highly satisfactory contribution to science,
to the second, which will also invite investigation and repay perusal.

M. Scipio Gras first lays down his theory and refers to existing
instances in its support, and then cites a new proof.

He states his view to be—that the causes usually assigned for the
abnormal condition of the Alpine strata are wholly gratuitous, and
that these strata were actually deposited in the order in which they
now appear,—that they have not been reversed,—that they constitute
a special paleontological province, originally differing from others by
reason of the enormous local contemporaneous disturbances.

His new case is taken from the valley of Entremont, where beds
containing White-chalk fossils are actually interstratified with others
of Neocomian age.

The geology of this district had previously been described by MM.
Fayre and Lory, who had attributed the phenomena to reversals and
faults; but M. Gras by a minute survey has been led to believe that
this is impossible, and that the intercalation of the two systems here
is real.

He concludes by stating that, ‘As these great differences, be-
longing not only to the fossils, but to the character and disposition
of the rocks, are not peculiar to the Upper Chalk alone, as compared

D2

18 GEOLOGICAL MEMOIRS.

with that of other countries, and of which we find parallel cases,
though not so well marked, in the rocks of Dauphine, it is probable
that these numerous anomalies spring from a common source,—that
is to say, the former existence of special geogenic centres, under the
influence of which the Alps were formed, and which render them a
geological province altogether unique.” [S. R. P.]

Srupies on the Mrtamorpuism of Rocks.
By M. Drtesse.

[Etudes sur le Métamorphisme des Roches, par M. Delesse. Ouvrage couronné

par Académie des Sciences. Paris, 1861.]
Tue author haying in a previous essay (Annales des Mines, 5 serie,
t. xu. 1857, p. 80) treated on special or contact metamorphism,
restricts himself in the present memoir to general or normal meta-
morphism. This work being of considerable length and replete with
facts, space will only permit of a general outline of the more important
conclusions. His definition of metamorphism is, the passage from
the fragmentary and amorphous state in which stratified rocks are
usually deposited, into one more or less crystalline; which change
may take place in rocks of every description. According to this
definition, some rocks must be considered metamorphic which the
majority of geologists have not looked upon as such,—as, for example,
deposits of clay in the midst of which crystals of selenite have been
subsequently developed.

The plan adopted by M. Delesse is, first to investigate and de-
scribe the nature of various rocks as now formed or as they occur
in an unaltered condition, and then to consider what changes have
taken place when they are metamorphic and crystalline. He thus in
Section 1 treats of beds and veins of minerals having a metallic basis,
as iron, manganese, zinc, copper, tin, &c.,—the general conclusion
being that, “‘ when subjected to general metamorphism, their struc-
ture becomes more crystalline. As to their chemical composition, it
is sometimes modified (by removal or addition of constituents) ; and
sometimes, on the contrary, it remains the same” (p. 23).

In Section 2 he considers the metamorphism of erupted rocks, and
suggests that the absence of rocks identical with modern volcanic
products, from crystalline schists, may be explained by supposing that
theytoo have been altered. Thus, for example, the operation of general
metamorphism may have changed trachyte into granite, and trap-
pean rocks into dolerite. Nevertheless he does not suppose that all
plutonic rocks have been produced in this manner, and shows that
they were often formed under the conditions which brought about
general metamorphism, and therefore, if again subjected to the same
influence, would be only slightly altered.

Section 3 treats on the metamorphism of stratified rocks, and in
the first place, on that of coal and other combustibles. The changes
which they have undergone when subjected to general metamorphism
are precisely similar to what are met with when beds of coal are in

DELESSE—-METAMORPHIC ROCKS. 19

contact with erupted non-voleanic rocks. There has been a gradual
elimination of the oxygen and hydrogen, and there is a gradual
passage from wood, lignite, and coal, to anthracite and graphite ; which
latter mineral, according to the author, is always associated with
rocks that have been subjected to an energetic metamorphic action.

In treating of the various accumulations of sulphate of lime, though,
as already mentioned, he looks upon the development of crystals of
gypsum in clay as acase of genuine metamorphism, he clearly points
out that some highly crystalline accumulations of gypsum were pro-
bably deposited as such, and are therefore in anormal condition. He
calls attention to the development of mica in some of the metamor-
phic gypsum of the Alps, which is of interest as showing that that
mineral may be formed at a temperature no higher than 120°C. (248°
F.), at which gypsum passes into anhydrits. In explaining the
origin of quartzite, the author specially refers to those sandstones
which consist of minute crystals of quartz, either deposited as such
or formed tn situ, showing that, in some circumstances, quartz may
erystallize when other rocks associated with it have undergone no
change.

It would render this extract too long if anything more than a
general outline were to be given of that part of the essay treating
on the changes which have taken place in the various kinds of sand-
stone and clay. ‘The author considers the case of sandstone, clays,
magnesian clay, marl, argilite and marnolite (Cordier), and the
various rocks to which they have given rise. Thus, sandstones
were changed into quartzites or quartzose mica-schist; clay into
chiastolite-slate; magnesian clays into talcous, serpentinous, or
chloritic schists ; and marl into pyroxene, garnet, or epidote-rock.
Argilite and marnolite have given rise to various rocks, according to.
the original character of the deposit or the degree of the subsequent
changes, beginning with slate, and finally terminating in mica-schist
and gneiss. Amongst these rocks he includes a number in which
crystals of felspar have been developed, and classes them with the beds
in Wales described as “ trappean ash” by the Geological Surveyors of
Great Britain. To gneiss is ascribed a double origin, being in some
cases “‘incontestably stratified,” and im others “a well-characterized
eruptive rock.” It is thus a connecting link between these
two great classes of rocks, is ‘‘most intimately connected with
granite, and its origin is evidently the same. ... In reality it is only
a variety of veined granite the crystallization of which appears to
have been impeded. We are thus naturally led to admit that
granite itself is a metamorphic rock. The same conclusion applies
to the other plutonic rocks” (pp. 76, 86). The occurrence of gra-
phite in various schists and even in granite itself is ascribed to
organic bodies enclosed in the rocks previous to metamorphism.
M. Delesse, however, in the concluding division of his essay clearly
admits that some granites have been erupted. If, says he, “‘ meta-
morphism be very energetic, it gives rise at once to both metamorphic
and plutonic rocks. These latter, which appear to enjoy a greater
amount of plasticity, have very often behaved as erupted rocks. They

20 GEOLOGICAL MEMOIRS.

have been brought up again to the surface of the ground by internal
pressures, and have filled the fissures and crevices of the crust of the
globe in a state of veins or larger masses. But they are then no
longer in contact with the corresponding metamorphic rocks, nor with
those at the expense of which they were formed; this, moreover, is
the most habitual manner of occurrence” (p. 88). The author then
proceeds to point out that the plutonic rocks are often far too small
to account for the magnitude of the metamorphic actions, and that
even quartzite, mica-schist, and gneiss have sometimes been formed
when no plutonic rock is present. He therefore concludes that
plutonic rocks are the effect, and not the cause, of general meta-
morphism ; and adopting this supposition, concludes by pointing out
how it will serve to explain the variation in the character of granite
at a greater or less distance from its extreme boundary.

[H. C. 8.]

GerotoeicaL UnpErGRounD Map of Paris, gc.
By M. A. Dztzssz, For. Mem. G.S., c&e.

[Carte géologique souterraine de la Ville de Paris, publiée d’aprés les ordres

de M. le Baron G. E. Hausmann, Sénateur, Préfet de la Seine, conformément a
la délibération du Conseil Municipale du 8 Novembre 1857, et exécutée par
M. Delesse, Ingénieur des Mines, Inspecteur des Carriéres du Département de
la Seine, 1858. Dessinée par Al. Babinski. Exécutée en chromolith. (Eemercier)
sous la direction d’Avril fs, Rue des Bernardins 18. En vente chez F. Savy,
20, Rue Bonaparte, Paris.
Tuts is a geological map of Paris (lithographed and printed in
colours), on the scale of 15 millimetres to 100 metres; and it also
indicates, by means of contour-lines of certain colours, the surfaces
of the several formations beneath Paris, to the greatest depth
reached by borings.

It is accompanied by three sections :—one across Paris from E. to
W.., from the Barriére de Vincennes to the Barriére de Neuilly: the
other two are N. and 8.,—one on the eastern side, from the Barriére
d’Aunay to the Barriére de Charenton ; the other on the west, from
the Barriére du Roule to the Barriére de la Mothe Piquet. The
vertical scale is 45 millimetres to 100 metres, being three times the
horizontal scale.

The made ground (‘‘ remblais,” 7) and the drift (“ terrain de trans-
port,’’ d') being supposed to have been removed, the following forma-
tions (“ terrains”’) are seen on the map :—gypseous marls and gypsum
(g'), lacustrine limestone (/’), middle sands (“‘sables moyens,’’s!), marls
above the calcaire grossier (m’), calcaire grossier (p'), plastic clay (a’),
and the cretaceous strata as far as the eault (c'). This map differs
from ordinary geological maps in that it indicates the surfaces of
these terrains. If, says the author of the map, we were to raise one
after the other the terrains composing the subsoils of Paris, com-
mencing with the latest, we should disclose successively so much of
the surfaces as corresponds with each of these formations. To deter-
mine with precision these surfaces, we have chosen a particular bed

DELESSE—MAP OF PARIS. Al

to serve as a datum: it was necessary that this special bed should
present well-marked mineralogical characters, easily recognizable in
a boring ; and it is generally that one which forms the upper surface
of each terrain. For 7’ it is the lower surface of the made ground
(r); for d', the lower surface of the drift (d); for g', the bed of
gypsum (g); for /', the first bed of magnesian laminated clay below
the marine beds (2); gl indicates the beds of gypsum in the lacustrine
limestone; for s’ is chosen the first bed of greenish-grey sand, gs
being beds of gypsum in the sables moyens; for m’, the first bed of
the marls (m), gm being gypsum beds in the marls; for p', the bed
of rock, or, that failing, the first bed of calcaire grossier (p); for a’,
the first bed of clay (“ glaise ”) and the calcareous marls (a); for ¢ the
upper chalk or pisolitic limestone (c): from g to ¢ inclusive, the
datum bed is the upper stratum of the terrain. The calcaire grossier
becoming marly in the northern part of Paris, is not represented
with so much exactitude as the other terrains; nevertheless its sur-
face is indicated on the sections by dotted lines.

Each of the special beds has had its bearings tested by accurate
levellings and measurements made at certain points: hence all its
inequalities of surface can be represented on the map by horizontal
curves, of the same colour as that used to indicate the terrain to
which the bed belongs, but of a darker tint; they are 10 metres
apart. The horizontal curves of the drift represent the surface which
would be obtained on removing this formation; they are 5 metres
apart.

When a point has been determined by levelling, it is indicated on
the map by a red dot, by the side of which are inscribed letters and
figures (of colours corresponding to the terrains found beneath)
which show the depth at which each special bed has been reached
there. The gypsum beds have their thicknesses shown; but they
are too irregular to be defined by horizontal curves.

The figures given as measurements in the map and sections are
calculated from a datum-line 100 metres below the mean sea-level.

By the aid of this map and the great mass of exact information
which it clearly gives as to the relative position and thickness of
the several strata, any one may calculate approximately the depth
at which each formation may be reached at any spot in Paris.

The level of the water, both subterranean and that of the river, is
shown in the sections by a blue line and figures. It has been deter-
mined by the drainage-works carried on in August 1857.

The numerous underground works carried on in Paris, during the
last few years especially, have all been turned to account in gaining
as exact a knowledge as possible of the nature of the substrata. For
the greater depths the author has had recourse principally to the
borings executed by MM. Mulot and Degousée. The plan of Paris
on which the map is based was published in 1856 by the Engineers
of Bridges and Roads of the Municipal Service. [T. R. J.]

22 GEOLOGICAL MEMOIRS.

HyprontocicaL Map of Paris, ge. By M. A. Detxssz, For. Mem.
Geol. Soc. &e.

[Carte hydrologique de la Ville de Paris, &. &. Par M. Delesse, &e., 1858.]

Tus is a chromolithographed map of Paris, of the same size and
form as the foregoing (p. 20) ; it is accompanied by the same sections,
and exhibits both the hydrographical and geological features of the
area. This map, to the execution of which the author* has devoted
nearly eight years, is constructed on novel principles. First, it
gives the relief of the ground by horizontal curves ; consequently it
indicates how the water runson the surface. Further, it shows the
sheets of subterranean waters beneath Paris. Their contours
and their flow are represented by horizontal curves a metre apart.
These curved lines have been traced according to the measurement of
the level of the water ina great number of wells; and therefore are
not hypothetical. Indications are also given of the quality of the
waters in Paris; and in this the author has had recourse to a plan
used in England—namely, finding the quantity of soap used up in a
given quantity of the water experimented upon. The degree of
“hardness” thus obtained is inscribed on the map at the points where
the several samples of water have been taken. Lastly, this map isa
geological map of Paris; for it shows the formations which are
bathed by the sheets of water. If, for instance, we take the sheet
of infiltration water falling into the Seine, its upper surface bathes
different formations, which are indicated on the map by corresponding
colours. ‘It was interesting,” says the author, “thus to trace the
formations at the level of the subterranean water-sheet, as one sees
how it traverses the several formations, and how the chemical compo-
of the former depends on that of the latter.”

This map has been executed by order of M. Hausmann, Prefect
of the Seine, who has also charged the author with the construction
of another similar map, which is to comprehend the whole of the
Paris basin. These researches are connected with the undertaking
known as the Somme-Soude Project, which contemplates the supply
of good water on a large scale, by bringing the rivers of Champagne
to Paris.

M. Delesse considers that this plan of hydrological mapping
might be advantageously applied to mining districts where the
works are much interfered with by water: the right places for adits,
galleries, &c., would thus be easily fixed upon.

(PE. era

GrorocicaL Map of the Sournern Portion of the Una Movnrars.
Constructed in 1854 and 1855, by Capt. Mrexirzxy and Capt.
Anriporr, Engineers of the Corps des Mines.

Tuts is a Russian map, on the scale of 1 inch to 8 miles (English),

and is accompanied with several sections. Of these, three are parallel

* A letter from the author to Sir R. I. Murchison, V.P.G.S., has supplied
much information respecting this map.—Ebir.

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On a JuRasstc Deposrr containing FresewaterR Fisa and Insects

tn KASTERN SIBERIA. By M. Ep. p’E1cHwaxp.

[Sur un terrain jurassique a poissons et insectes d’eau douce de la Sibérie orien-
tale. Par M. Ed. d’Hichwald. Bull. Soc. Géol. de France, 2¢ série, vol. xxi.
1863, pp. 19-25.]

M. p’Ercuwatp refers to his observations, made in 1846, in his

‘Géognosie de la Russie,’ on freshwater strata in the district of

Nertchinsk, in Eastern Siberia, containing fossil Fish, described by

him as Pholidophorus macrorhynchus, associated with Posidonomya

and some larvee of Insects.

tn 1850* Dr. J. Muller proposed for this fish the name of Lyco-
ptera Middendorfir, regarding the shale in which it was found as of
Kocene age; while, on the other hand, M. d’Eichwald had considered
the strata as belonging to some member of the Jurassic system *.

A portion of this paper consists of notes upon the fossils occurring
in these beds. The Fish already mentioned he states to agree pretty
well generically with Pholidophorus, but better with dthalion of
Munster (1842), which Prof. Agassiz somewhat later classed as a
subgenus of Pholidophorus.

_ The remains of Neuropterous Insects accompanying the Fish the

author named Ephemeropsis trisetalis; with these occur Estheria Mid-

dendorfii, Jones, Paludina pura, D’Kichwald, and a small species of

Cyclas. He next remarks, that up to the present time the relative

age of the shale has not been satisfactorily determined. It readily

splits ito very thin layers, between which are found, in great
numbers, dthalion (Pholidophorus) macrorhynchus and Estheria,
whilst Ephemeropsis, Paludina, and Cyclas are sparingly met with.

The shale is found to pass into an argillaceous schist, a rock which

constitutes everywhere in Eastern Siberia the highest mountains.

It is doubtful, however, whether this is the same schist which con-

tains fossil Fish upon the banks of the River Tourga, and is pro-

bably of older date; it is generally devoid of fossils, but forms allied
to some Liassic species of Monotis, that occur in the Tyrol, are some-
times met with.

The schist occupies the eastern shore of the Gulf of Oxhotzk,
and contains Monotis Ochotica, Keys., with its several varieties, which
were named by Keyserling MW. minor, M. media, and M. major
respectively. It may therefore be regarded as a passage-bed to the

* Middendorf, ‘ Voyage en Sibérie,’ p. 261.
+ See also Quart. Journ. Geol. Soc. vol. xix. pp. 71 e¢ seq.

VOL. XX.—PART II. D

22 GHOLOGICAL MEMOIRS.

Lias of the Tyrol, which as a marine sediment may be contempo-
raneous with the Jurassic strata of the Tourga, which were deposited
in a freshwater lake of very considerable extent.

He further adds his belief that Jurassic limestone is clearly
developed in Northern Siberia and in the Islands of the Arctic Ocean.
as previously noticed by him, in 1841, in his memoir upon the
Ceratites of the Muschelkalk of Kastern Siberia, (Re

On the Grotoey of Atpanta. By Dr. A. Bovs.
| Proceed. Imp. Acad. Vienna, January 21, 1864.1

Berorr the year 1859, the Albanian River Drin flowed to the
Adriatic through the valley of Zadrima and the limestone-clifts of
the defiles of Baldrin and Lesch. In 1859 an inundation of this
river, probably simultaneous with another of the River Kiri, caused
the Drin to work out from its north-west source in the Skela Moun-
tains a new course through cultivated lands, down to its junction
with the Kiri, which falls into the Boyana. The Rivers Devol and
Scumley,in Middle Albania, separated only by a large plain, without
any mountains or hills, likewise unite during periods of inundation,
at least at the narrower part of this isthmus. Westward, a small
hilly portion remains, like an isle between the sea and the two
rivers. Between the basin of Scutari and the Gulf of Arta, and still
more to the south, a broad band of land is exclusively occupied by
Tertiary deposits overlying an old depressed formation of Secondary
limestones, which appear through the Tertiaries only in some few
places. Eocene strata are prevalent in Epirus ; Miocene and Neogene
in Northern and Central Albania. A fine section of these deposits
is to be met with on the southern slope of the Graba-Balkan. On
this slope, the Nummulitic Limestone is overlain by a thick deposit
of blue argillaceous marls. Above this, strata with Cerithia and
Neritine, such as are not met with in the Vienna Basin, are to be
seen. The uppermost deposit is a thick layer of quartzose Leitha-
conglomerate (Neogene). As in Istria, only on a larger scale, the
Kocene deposits in South Albania comprise two great subdivisions ;
the Nummulitic limestone forms the high ground, and the marls and
sandstones occupy the depressions and erosions, both being overlain,
in some of the larger valleys, by freshwater limestones and alluvium.
Several sulphurous hot springs are known to exist in North Albania,
and it may be worth notice that there, as at Baden, near Vienna,
gypsum occurs imbedded in Secondary limestone. [Count M.]

On the Coat-pepostts of Gross-Ramine (Urprr AvstetA).
By Baron STeRNBACH.

[ Proceed. Imp. Geol. Instit. Vienna, February 16, 1864.]

Five seams of this Coal, of which only the third, about 3 feet
thick is profitably worked, are imbedded in alternately compact and

ZITTEL—BIVALVES FROM GOSAW. 23
friable shales, interstratified with grey micaceous sandstones of
Lower Liassic age. The shales forming the floor of the second seam
include ferruginous marls with vegetable impressions, among which
Camptopteris Wilsoni prevails, while in the shales of the roof Peco-
pteris Whitbyensis is the predominant form, though specimens of
Teniopteris vittata have also been met with. Some layers of the
imbedding rock are full of organic remains ; for instance, Plewromya
unionides, Pecten infra-lassicus, Gonomya rhombifera, Panopea
liassica, &e. The mining-operations, after having been carried
through barren rocks and several unprofitable Coal-seams, at last
led to the opening of a coal-seam 9 feet thick, of which from 5 to 6
feet are good laminated coal, giving 60 per cent. of coke and only
20 per cent. of ash. At several places the workings reached as far
down as the variegated Liassic marls. [Count M. |

On the Neocenr Depostts of the Vatuxys of the Mtrz and Mur
(Styria). By Herr D. Srour.

[ Proceed. Imp. Geol. Instit. Jan. 19, 1864.]

Two horizons differing in age may be distinguished in these deposits,
the upper portion of the more ancient consisting of conglome-
rates, with hollow pebbles, and sandstones; and the lower part of
shales, with sometimes considerable coal-seams; both subdivisions
contain remains of Mastodon angustidens, Dinotherium Bavaricum,
and other Mammals. This older series may be equivalent to the
marine strata of the Vienna basin. It is overlain by plastic clay,
with occasionally very considerable coal-seams, both containing
intercalated beds made up in places almost entirely of Congeria
triangularis, Partsch ; they are certainly equivalent to the uppermost
freshwater strata of the Vienna Basin, and are succeeded by an
extensive gravel-deposit. [Count M.]

On Bivatves from Gosav. By Dr. Zrrret.
[ Proceed. Imp. Acad. Vienna, December 10, 1863.]

Tue Gasteropods of this highly interesting deposit have been described
by Dr. Zékély (Jahrb. k.-k. geol. Reichsanst. 1852). Subsequently
Prof. Reuss published descriptions of the Corals and Foraminifera.
Chev. von Hauer those of the Cephalopods, and Dr. Stoliczka those of
some freshwater Gasteropods from the same locality. Dr. Zittel, of
the Imperial Museum of Vienna, has lately published descriptions
and figures of seventy-three species of Gosau Dimyarian Bivalves,
all of which belong to known genera, stated (with the exception of
Cyclina) to occur in Cretaceous deposits. The greater number of the
species are new, and only a few have been hitherto met with in other
localities. Of the 73 species, only 17 have been found (most of them

24 GEOLOGICAL MEMOIRS.

in Southern France) beyond the Austrian Alpine regions; all the
others (6 of which had been previously described by Sowerby and
other authors) are confined to the Gosau strata, in the strict sense of
the term. The species of Unio, Cyclas, and Cyrena which Dr.
Stoliczka found, associated with Gasteropods, between the coal-seams
of the Wand, near Wiener-Neustadt (8. of Vienna), are of particular
interest as members of an ancient freshwater fauna, the former
existence of which has been recently confirmed by the discovery of
gigantic Saurian remains. [Count M. |

On some GEOLOGICAL Sections 7 the TRatsentHAL (LowER AvstTRIA).
By M. Lrpoxp.

[ Proceed. Imp. Geol. Instit. Vienna, March 15, 1864.]

THeEsE sections exhibit the following succession of strata, in ascend-
ing order:—(1.) Werfen beds, with Myacites Fassaénsis and other
characteristic organic remains. (2.) Rauchwackes. (3.) Dolomite,
dark-coloured and partly bituminous. (4.) Guttenstein beds, black
spathose limestones, with Ceratites Cassianus. (5.) Nodular black
or light-grey limestones, containing nodules of chert, alternating
with black, thinly schistose limestones, including Ammonites Aon and
Halobia Lommelithe Gossling beds. (6.) Sandstones and shales
with intercalated coal-seams; shales with impressions of vegetables,
as Pterophyllum longifolium, Equisetites columnaris, Pecopteris
Stuttgartensis, &c.,and overlain by slates with Posidonomya Wengensis,
and a thin bed of limestone with Ammonites floridus—ILnunz strata.

7.) Black or brownish, partly dolomitic, limestones, in thin layers,
with Pecten filosus, Corbis Mellingi, Perna Bouei?, Myoconcha, &c.,
and above therfi similar light-coloured limestones with Myophoria
Whatleye, Cardita crenata, &c., overlain by dolomites—Opponitz
strata. (8.) K6ssen beds, overlain by (9.) Hierlatz strata near
Sihenfield, and by Liassic variegated marls with Ammonites near
Traisen. (10.) Red Jurassic limestones (Klausen beds) with Am-
monites triplicatus. (11.) Upper Jurassic Aptychus-slates and lime-
stones. (12.) Neocomian strata.

The Lower (Alpine) Trias is represented by the deposits Nos. 1
to 4, the Upper (Alpine) Trias by Nos. 5 to 7, the Alpine Lias by
Nos. 8&9. The whole of the Coal-deposits in the lower part of the
North-east Calcareous Alps are interstratified with the Upper Trias,
while those on the southern margin of the Vienna-sandstone zone
are subordinate to the Gresten (Middle Lias) beds. [Counr M.]

MEGLITZKY AND ANTIPOFF—S, URAL. 22

E. and W. sections across the country, with the heights determined
by the barometer, and on the scale of 1 inch to 16 miles horizon-
tally ; and fourteen are smaller uncoloured local sections.

The following formations are indicated by colours on the map and
long sections:—A. Silurian. Green and grey sandstone and conglo-
merate; green, grey, and other argillaceous schists and quartzite.
(Obolus Apollinis, Lingula oblonga, Orthis calligramma, O. testudi-
naria.) B. Devonian. Limestone, grey and white ; calcareous sand-
stone (Brook Pismianka), and schists. (Terebratula elongata, T. Ari-
maspus, T. aptycha, T. Pugnus, T. cuboides, Spwifer Tenticulum,
Sp. muralis, Sp. Archiaci, Orthis resupinata, Avicula reticulata, Pen-
tamerus galeatus, Je.) C. Carboniferous. Grey clay and schist (Pe-
copteris, Cyclopteris, Voltzia, Sphenopteris, Neggerathia, §c.). Ferru-
ginous Sandstone. Yellow, grey, and black limestones, argillaceous
schist, and grey and yellow sandstone (Goniatites, Fusulina cylindrica,
Spirifer Mosquensis, Sp. striatus, Productus antiquatus, P. punctatus,
P. giganteus, Cyathophyllum, §c.). D. Permian. Red sandstone,
conglomerates, clays, and limestones. E. Cretaceous. White and
yellow clays, sandstones, and conglomerates (Belemmtella mucronata,
Terebratula carnea, T. elongata, Rhynchonella octoplicata, Ostrea
vesicularis, ge.). EF. Alluvial clay and sand. G. Igneous rocks:
a, granite, granito-syenite; 6, diorite and porphyry (greenstone and
felspar-porphyry); ¢, serpentine; d, quartz-veins. H. Metamor-
phie rocks: 1. mica-, talc-, and chlorite- schists; 2. conglomeratic
schist and jasper.

The auriferous sands are also marked (by a yellow line), and the
numerous points where astronomical and barometrical observations
were made are also indicated. The barometrical stations are used
to indicate the lines of section; on the latter the heights are given
in English feet.

The smaller sections are :—Fig: 1. Curved strata of Silurian sand-
stone and argillaceous schists on the banks of the Brook Maloi Su-
riane. Fig. 2. The Turate Mountain, showing Silurian sandstone,
limestone, and schist, and conglomeratic schist. Fig. 3. The Si-
lurian sandstone and clay-schist on the River Arantache. Fig. 4.
The Silurian beds (sandstone and clay-schist, with breccia and jas-
per) on the banks of the Brook Gusicha. Fig. 5. Section at the
village of Verchneosernoy, to the east, showing the beds of the Car-
boniferous Limestone, alternating with sandstones and conglomerate.

Fig. 6. Section at the village of Griasnuschinskoy, showing the
strata of Carboniferous Limestone (a—c), the Silurian rocks (alter-
nations of green and grey sandstone, clay-schists, and conglomerate),
and dykes of diorite(g). Fig. 7. Strata of the Carboniferous Lime-
stone at the Factory of Kananicolsky, to the west (a, sandstone ;
b, grey and black limestone; c, Fusulina-limestone ; d, Encrinital
limestone; e, calcareous sandstone; f, limestone with Productus
antiquatus, P. punctatus, Spirifer Mosquensis, fc.; g, limestone
with Cyathophyllum, &c.; h, argillaceous and pebbly. schists ; and 2,
Silurian rocks). Fig. 8 shows a complete section of the Carboni-
ferous, Silurian, and Metamorphic rocks at the Factory of Preobra-

VOL XVII.—-PART II. 13

24 GEOLOGICAL MEMOIRS.

gensky, to the west :—a, sandstone; 6, grey and black limestone ;
c, Fusulina-limestone; d, Encrinital limestone; e, sandstone; /;,
limestone with Productus striatus, Spirifer Mosquensis, §¢.; 9s
limestone with Cyathophyllum, ce. ; h, argillaceous and conglome-
ratic schists; 2, Silurian sandstone and schist; %, conglomerate ;
1, tale-schists; m, mica-schists; », serpentine-dyke; p, conglo-
meratic schists (locally overlying the mica-schist); q, quartz-veins.
Fig. 9. Carboniferous strata on the banks of the River Maloi Urta-
sime:—a, grey and black limestone ; 6, ycllow limestone, with En-
crinital limestone (c); d, conglomerate; ¢ & f, alternating clay-
schist and sandstone ; g, limestone with Cyathophyllum, fe. Fig. 10.
Carboniferous Limestone on the porphyries on the banks of the River
Verchniaia Orlofka:—a, porphyry; 6 & c, strata of Carboniferous
Limestone, with abundant fossils, and not at all metamorphosed ;
d, dykes of diorite in the porphyry. Fig. 11. Carboniferous Lime-
stone on the Brook MaloiSuriane. Fig. 12. Contorted strata of Car-
boniferous Limestone near the village of Kugartschi.

Fig. 13. Cretaceous strata :—a, white and yellow clay with seams
of sand (Belemnitella mucronata, Terebratula carnea, T. elongata,
Rhynchonella octoplicata, Ostrea vesicularis, gc.) ; b, sandstone and
conglomerate with chlorite. Fig. 14 is a section of the Michailavsky
bed of gold-bearing sand on the banks of the Brook Suvundue :—
a, grey Carboniferous Limestone; 6 & c, alternating argillaceous
schist and sandstone below the limestone; e, quartz-vein through
the limestone; d, superficial auriferous sand.

[Tan

On the Moxasse of Sournern Bavarta. By Franz R. von Haver.
[Proceed. Imp. Acad. Vienna, January 3, 1861.]

Arter a close examination of the Prien Valley, which opens into the
Chiem-See, Prof. Emrich admits five subdivisions of the South Ba-
varian Molasse. The lowest is of marine origin, and paleontologi-
cally parallel to the strata of Alzey on the Rhine. This is imme-
diately overlain by the lignitiferous freshwater or brackish strata of
Miesbach. The third or middle subdivision (Conchiferous Molasse),
of marine origin, with organic remains identical with those of the
Swiss marine Molasse, is overlain by strata containing fossil forms
characteristic of the marine deposits of the Vienna basin. The fifth
or uppermost subdivision is characterized by the presence of fresh-
water Univalves, Melanopsides and Neritine. [Count M.]

On the Drevontan and CarnontreRovus Rocks of Moravia.
By MM. Worr and Lirotp,

[Proceed Imp. Geol. Instit. Vienna, February 26, 1861.]

Mrssrs. Wotr and Lirorp, at the request of the “ Wernerian So-
ciety” of Briinn, surveyed in the autumn of 1860 the environs of

PT

VON HAUER—TRANSYLVANIA. aa

Olmiutz, Eastern Moravia. Crystalline rocks (granite, mica-schist,
argillaceous slates, syenite, phyllites, and varieties of quartzite),
overlain by extensive paleozoic deposits, are prevalent in the space
comprised between Briinn, Boskowitz, and Olmiitz. Semicrystalline
limestones, including beds of brown iron-ore (Baron Reichenbach’s
« Lathon ”’) are intercalated between the uppermost crystalline and
the older paleeozoic rocks. The nature and subdivisions of these last
rocks have been lately better cleared up by the discovery of some
fossiliferous localities. The oldest palzeozoic strata are overlain by a
zone of limestones, 4 to # of an Austrian mile in breadth, in fantasti-
cally shaped groups, probably the remains of a once contimuous
mountain-range. The presence of Stringocephalus Burtini, a cha-
racteristic Lower Devonian form, allows this limestone to be paral-
lelized with those of the Hifel in the Rhenish System. A narrow zone
of red-and-green-spotted marbles may represent the Clymenian
Limestone of the Upper Devonian series.

Over these lower strata a complex series of alternating slates and
sandstones, comprised hitherto under the general denomination of
“‘ Greywacke,” form an extensive plateau, separated northward from
the higher subdivisions by a considerable depression, and sloping
eastward by degrees towards the Miocene and Diluvial deposits.
Some of these slates are worked on an extensive scale between
Olmiitz and Troppau.

Paleontological investigations have now ascertained that this
whole group, hitherto known as Greywacke, belongs in reality to the
lowermost portion of the Carboniferous series, and is analogous to
the so-called “‘ Kulm Strata.” Prof. Goppert had already inferred,
from the vegetable remains found in it (especially from Calamites
transitionis), its analogy with the “transition ” deposits of Hayni-
chen (Saxony) and with the Posidonomya-slates of Nassau,—a view
subsequently confirmed by the discovery of other vegetable remains
and of Goniatites Crenistria, and recently fully established by the dis-
covery of a most characteristic fossil form, the Posidonomya Becher.

limestones of the Upper Jurassic series occur near Brinn and
Blansko. [Count M. }

On the Motntains South of Kronstapt, TRANSYLVANIA.

By Franz Rirrer von Haver.
[ Proceed. Imp. Geol. Instit. Vienna, February 26, 1861.]
Tue orographical features of this group are quite different from
those of the neighbouring mountains of Fogaras. Instead of a
uniform longitudinal range, they offer the aspect of colossal massifs,
sometimes with extensive plateaux, isolated from each other by deep
valleys, running irregularly in every direction, and sloping towards
the plains and the lower mountain-region at uncommonly steep
angles, so as to form precipices several thousand feet deep. The
altitude of these massifs varies generally between 4100 feet and 5700
feet; the two highest among them rise, one to 7050 feet, and the
other to 7900 feet.

26 GEOLOGICAL MEMOIRS.

A white limestone, probably Jurassic, forming cliffs of grotesque
configuration, and joining north-westwardly the crystalline slates of
the Fogaras Mountains, is the prevailing rock in this mountain-
group. Organic remains lately found by Mr. Stur (among them
ERhynchonella plicatella, Sow., and Terebratula spheroidalis, Sow.)
are indicative also of the presence of the Brown Jura, a subdivision
the existence of which in Transylvania was hitherto unknown.
Next to the White Jura in extent and importance, come conglo-
merates of primary rocks, and sometimes enormous boulders of the
white limestones occurring in some isolated localities around Kron-
stadt. These conglomerates remind us, by their prevalent greenish
tints, of the greenish Eocene sandstones of the Alps, and are so con-
nected with the other undoubtedly Kocene conglomerates around
Kronstadt that they must be consequently ascribed to the same early
Tertiary period.

A sandstone, seeming to dip beneath the before-mentioned Jurassic
strata, includes organic remains belonging, as far as they are as yet
recognized, to the Upper Cretaceous fauna. Forms characteristic of
the Lower Cretaceous (Neocomian) strata, as Belemnites dilatatus,
De B., anda large tooth of Spherodus (probably Spher. Neocomiensis,
Ag.) have been found among the organic remains of Vallye Drakuluj
near Kronstadt. iCaaenNten

On the Larce Tertiary Carnivora of Austria.
By Prof. E. Suzss.

| Proceed. Imp. Acad. Vienna, March 7, 1861.]

Tne Tertiary and Post-tertiary deposits, so important on account of
their organic remains in throwing light on the question, how far
the repeated changes undergone by organic creation are the effects of
changes in the external condition of life, have been during a number
of years an object of sedulous investigation to the paleontologists of
Vienna, and especially to Prof. Suess, who, at the expense of the
Imperial Museum, explored in 1860 the western borders of the
Vienna basin, and caused the ossiferous deposits of the Baltavar,
near Eisenburg (W. Hungary), to be thoroughly searched on an
extensive scale. This locality, first discovered by M. von Schwaberau,
corresponds in its general features with the well-known deposit of
Pikermi, near Athens, comprising remains of Machairodus, Hyena,
Antilope, a gigantic species of Giraffe, and many other genera. The
determination of the Baltayar fossils has been effectually assisted by
a rich collection of Pikermi fossils lately presented to the Imperial
Museum by Count Breuner-Felsach, formerly Austrian Enyoy at
the Court of Greece. Prof. Suess in his paper describes three species,
Machairodus (a genus analogous to the Lion of the present period),
Hyena evimia, and Amphicyon intermedius—an animal similar to the
Wolf, only larger in size. [Count M. |

TRANSLATIONS AND NOTICES

OF

GEOLOGICAL MEMOIRS.

On the SrRaTIGRAPHICAL Succession of the Bups in the Savoy ALps.
By M. Cu. Lory.

{Note sur la constitution stratigraphique de la Haute-Maurienne, par M. Ch.
ae Bulletin de la Société Géologique de France, deuxiéme série, vol. xviil.
p. 34.

Tue subject referred to in an abstract contained in the ‘ Quarterly
Journal,’ vol. xvii. part 2. (Miscell.) p. 16, has received further eluci-
dation in the communication of M. Lory, who confirms the deductions
of M. Favre, and considers that the discovery of the Nummulitic
strata underlying the Lias proves the reality of the great overthrow
which has reversed and replicated the strata in a manner astonishing
even to those best acquainted with similar minor phenomena else-
where. M. Lory has given general sections of the structure of the
Alps ;.and M. Favre adds a letter and section giving full details of
the striking instance of reversal on a grand scale shown in the
district of St.,Jean de Maurienne, which will henceforward become
a typical instance.

fiSe des, JEG]

On the Patmozorc Rocks of Brnerum and the Norru of France.
By M. Jurxs GossELer.

[Mémoires sur les terrains primaires de la Belgique, des environs d’ Avesnes et
du Boulonnais, par Jules Gosselet: Paris, 1860. Also ‘‘ Observations,” c.,
Bulletin de la Société Géologique de France, deuxiéme série, vol. xvii. p. 18.]
M. GosseLer has now occupied several years in the careful field-work
and study, the results of which are embodied in his Memoir of 1860.
In the subsequent communication to the Society, he gives a résumé
of the work. A short abstract of both will justify us m welcoming
this valuable addition to paleeozoic literature, especially in regard to
that portion of it which affects the relationship of the uppermost
Devonian beds to the Lower Carboniferous system. After referring
to the history of the inquiry and paying a just tribute to the excel-
lency of the geological topography of Dumont, he states that he has
ascertained both stratigraphically and paleeontologically the existence
of eleyen principal divisions, which have a general correspondence

VOL, XVII.—PART II. F

28 GEOLOGICAL MEMOIRS.

with the divisions of Dumont. These are (reversing his order for
the sake of naturalness, though not altering the enumeration)—

I Coal=eritsvand shales 230. eer ene

2. Upper Carboniferous Limestone (Visé) .... + Carboniferous.
3. Lower Carboniferous Limestone (Tournay) .

4, Psammites of Condros ..........
Ss plates! ofbamenme ee Gok! ene
Oo Gavetilimestomel sme eee Middle
“i. Calceolacslates (a2 4. 6 tein >Devonian.
oy bumnot conglomerate a7.) ) ace
9. Grauwacke with LeptenaMurchisoni
10. Conglomerates and roofing-slates
11. Slates and quartzites, with porphyry........ Silurian. |

Lower

No. 1. The productive coal-measures offer nothing worthy of re-
mark save the author’s conclusions in favour of the opinion that the
coal-basin of the Boulonnais is the prolongation of that of Mons,
and is not a bed in the Lower Carboniferous series. His reasons will
be found in the Memoir, p. 132.

No. 2. M. Gosselet considers that there is sufficient paleeontologi-
cal evidence for the division (first suggested by M. de Koninck) of
the great mass of limestones and shales below the coal into two
groups, typified by the limestones of Visé and Tournay. He thus
characterizes the former in Belgium :-—

Alum-shales and limestones with Productus carbonarius and
Goniatites diadema.

Limestones with Productus undatus. :

Productus-limestone. Productus giganteus, P. sublevis, and P.
cord.

Dolomites.

No. 3. Lower Carboniferous Limestone. Tournay.

Nodular or cherty limestone.

Crystalline limestone. Spirifer mosquensis and Sp. semireticu-
latus.

Black limestone with Productus Hebert.

No. 4. Condros psammite.—Between the Carboniferous Limestone
and that of Givet there occurs a great series of coarse slates, grits,
and sandstones, which M. d’Omalius d’Halloy designated by this
name. Dumont separated from them the schists of Famenne; and,
though he afterwards abandoned the division, M. Gosselet considers
it established. There are several stages of No. 4; but the upper-
most Devonian rocks, the Cypridina- and Clymenia-slates, appear to
be everywhere absent. The upper beds at Oetrungt are charac-
terized by Phacops latifrons, Terebratula concentrica, T. hastata, T.
Bolonensis, Spirifer Vernewliu, Orthis crenistria, O. arachnoidea, and
Productus scabriculus. The whole group, wherever lime is present,
is abundantly rich in fossils, amongst which Sp. Vernewilii plays the
most considerable part.

No. 5. The schists of Famenne are the same as are designated in
the communication to’ the Society the TYerebratula cuboides beds.

GOSSELET— PALAOZOIC ROCKS. a

They are well displayed around and within Fort Condé, near Givet,
as follows :—

Greenish schists with Spirifer Vernewli.

Black schists with Cardium palmatum.

Schists with limestone-nodules and Terebratula cuboides.

Blue limestone.

Schists with Receptaculites and Terebratula equiconvexa.

No. 6. The great Givet limestone is identical with that of Paffrath.
Its characteristic fossils are Macrocheilus arcuatus, Huomphalus
rotula, Rotella heliciformis, Murchisonia coronata, and Stringocephalus
Burtini. Different stages are characterized by different Spirifers.
At Macon (near Chimay) and in the Eifel, Phacops latifrons, Ortho-
ceras nodulosum, Gomphoceras inflatum, Lucina proavia, and Penta-
merus formosus occur.

No. 7. This is a series of argillaceous schists with intercalated
limestones characterized by Calceoia sandalina, Spirifer speciosus,
Pentamerus galeatus, and Terebratula primipilaris. In other places
Chonetes minuta, Spirifer cultryjugatus, and Leptena depressa occur
in different beds of this series.

No. 8. This is a great development of red conglomerate and sandy
grits, comprising paying-stone beds barren of fossils; but M. Hébert
reports. having found at one place within its area Dolabra Har-
dingu, Avicula fasciculata, Productus Murchisonianus, and a Spirifer
like Sp. Bouchardu.

No. 9. This is the “‘Coblentzien” of Dumont. The coarse rock
to which the well-known and little-liked term of “‘ grauwacke”’ is
attached contains Pleurodictyum problematicum, Leptena Murchison,
and some Terebratule.

No. 10. Lastly, the Devonians terminate downwards in a great
series of rocks, principally conglomerate, called by Dumont “ gédi-
nien,” and separated stratigraphically and mineralogically into five
divisions, one of which is fossiliferous and contains Dalmanites,
Homalonotus, Grammysia, two small Spiriferi, Chonetes sarcinulata,
two species of Orthis, Colaster constellatus, and Tentaculites ornatus.

No. 11. This is the ‘“ Ardennais” of Dumont (comprising three
large divisions well characterized mineralogically), which, though at
present barren as to fossils, is usually agreed to be Silurian from its
position.

The Memoir contains the author’s views as to the correlation of
these groups with the Paleeozoics of other countries, copious lists of
fossils, and is well illustrated by sections.

It is quite evident that the Lower Devonian rocks are so well cha-
racterized in Belgium that we may obtain from them considerable
light on our own more fragmentary and disturbed deposits. By
identifying one band of the Plymouth limestone with that of Givet,
we may obtain a useful horizon for the middle of the great marine

group constituting the western extremity of our own island.
[S. RB. Po]

30 GEOLOGICAL MEMOIRS.

On the AccumuLation of Detnitus in the STEINFELD.
By Lieut.-Col. Jonxxar.

[ Proceed. Imp. Acad. Vienna, March 14, 1861.]

Tue plain called “ Steinfeld ” near Wiener-Neustadt (8. of Vienna)
is in reality a flattened conoidal accumulation of detritus, the apex
of which lies at Wollersdorf at the mouth of the Piesting Valley,
from whence it slopes away in every direction, the angle of incli-
nation being least in the direction of Pottendorf. The maximum
length (2 Austrian or about 10 English miles) is between this place
and Wollersdorf; the maximum breadth (13 Austrian or about 74
English miles) is between Neustadt and Leobersdorf. There can be
no doubt that the whole accumulation has come out of the Piesting
Valley. A number of careful measurements make its volume to
be 450,387,000 cubic fathoms (the fathom being equal to 216 cubic
teet)—about 51, of the cubic contents of the whole Piesting Valley,
calculated to be 9033 millions of cubic fathoms. If the proportional
densities of the detritus and of solid limestone are taken into con-
sideration, the total mass of this accumulation of detritus may
amount to the thirtieth part, in volume, of the quantity of solid
limestone required to fill up completely the Piesting Valley in its
present extent. [Count M.]

On the Havyinr-rock of TRANSYLVANIA.
By K. Rrrrer von Haver and Director W. Harprnerr.

[Proceed. Imp. Geol. Instit. Vienna, May 28, 1861.]

Specimens of hauyine discovered by M. Herbich near Ditro (Tran-
sylvania), have been analysed in the laboratory of the Vienna
Imperial Institute by K. Ritter von Hauer, who found them to con-
tain a notable quantity of chlorine, a substance also stated to occur
in sodalite. This circumstance, together with its granitoid erystal-
lization, assigns to the Ditro mineral its place among the mineral
species or varieties named Sodalite, Roselite, Ittnerite, Sapphinine,
Spinellan, Hauyne, and Lapis Lazuli. Its colour is between azure
and sky-blue ; its specific gravity 3°318 ; its hardness according to
Mohs’ scale 5:5 (between fluor-spar and felspar). The rock for
which Director Haidinger proposes the name of ‘* Hauyne-Rock ”’ is
a granular aggregate of hauyne, orthoclase, cancrinite, eleolite, and
oligoclase, interspersed with minute particles of black amphibole,
mica, magnetic iron, sphene, calcareous spar, &c. The whole com-
pound, when cut and polished, is conspicuous for its beautiful mixture
of blue, white, grey, and reddish-yellow tints, which, together with
its hardness, makes it, when polished, a very fit material for orna-
mental objects.

MM. Quaglio and Fritsch have begun the regular exploitation of
this new and fine mineral substance, and intend to send specimens
of it to the London Exhibition of 1862.

[Count M.}

ALPHABETICAL INDEX

TO THE

PROCEEDINGS OF THE GEOLOGICAL SOCIETY.

[The fossils referred to are described, and those of which the names are printed
in italics are also figured. |

Apzots Laney, Herts, flit imple-
ment found at, 367.

Acanthocladia anceps, 307.

Analysis of the lignite from the Valley
of the Souri River, 409.

Anatina ? precursor, 507.

? Suesst, 507.

Andes, Mr. J. W. Salter on the fossils
from the, 62.

Aneimites Acadica from Nova Scotia, 5.

Amniversary Address of the President,
xxxi-lsxu. See also Horner, L.,
Esa.

Annual Report, 1.

Anthrapalemon dubius, 532.

Grossarti, 580.

Arca? Brownii, 69.

Lycetti, 501.

Archzoteuthis Dunensis (Roemer),
Prof. T, H. Huxley on, 163.

Ardsheal Peninsula, Highlands of
Scotland, 266.

Arisaig in the Highlands, 203.

Ashdown Sand, 277.

Assyunt in the Highlands, 96.

Astacoderma bicuspidatum, 549.

declinatum, 550.

—— planum, 551.

remiforme, 551.

serratum, 550.

spinosum, 550.

terminale, 549,

triangulare, 550.

undulatum, 550.

Australia, the Rev. W. B. Clarke on
the plant-bearing beds of, 354.

Avicula contorta, 499.

Avicula contorta zone, Mr. C. Moore
on the, 483.

Avicula solitaria, 499.

Award of the Wollaston Donation-
Fund, xxx; Medal, xxvii.

Axinus cloacinus, 502.

eoncentricus, 502.

depressus, 502.

dubius, 305.

elongatus, 502.

Ballahulish in the Highlands, 266.

Banavie in the Highlands, 208.

Barkoi and Mahadewa Hills, India, 347.

Batheaston and Paulton, sections at,
492, 493.

Beann Taobhliath, 198.

Bedford, flit implements found near,
366; section across the Valley of
the Ouse at, 364.

Bedwins (Wiltshire), a reconstructed
bed on the top of the chalk near the,
527.

Beer-Crowcombe, Rheetic and Liassic
beds at, 485, 489.

Bellerophon, from Ilampu, 70.

Bengal, plant-beds of, 347; reptilian
remains from, 362.

Ben-y-Gloe Mountains, Highlands of
Scotland, 268.

Berks, reconstructed bed of chalk in,
527.

Beyrichia Forbesi, 67.

Biddenham (Beds), flint implements
found at, 366.

Blair Athol, 222, 262.

Blairgowrie, 226.

Bolivia and Southern Peru, Mr. D.
Forbes on the geology of, 7.

Boliviana bipennis, 72.

Melocactus, 71.

proboscidea, 71.

Bone arrow-head from the Montagne
du Ker, 4:70.

TNDEX TO THE PROCEEDINGS.

Bone-caves on the Montagne du Ker
at Massat, M. Alfred Fontan on two,
468.

Bone-caves in Languedoc, M. Lartet on
the, 473.

Boracic-acid deposits of Bolivia and
Peru, 13.

Borrodale, in Scotland, section at, 204.

Boulder on the plains south of Carlton,
sketch of, 396.

Boulders in West Rosewarne Mine,
517.

Breadalbane Forest, 215.

Brodie, the Rey. P. B., on the distri-
bution of the corals in the Lias, 151.

Brodsworth, Yorkshire, 313.

Bronn, Prof. H. G., award of the Wol-
laston Medal to, xxvii.

Brotherton, Permian beds of, 289, 316.

Bunbury, Sir C. J. F., Bart., notes on
a collection of fossil plants from
Nagpur, Central India, 325.

Bute, the older rocks in, 136.

Caledonian Canal, or Great Glen, Lower
Silurian rocks east of the, 205.

California, terraces in, 404.

Callender, Highlands of Seotland, 258.

Carabidze in the Rheetic beds, 513.

Carboniferous rocks of Peru and Boli-
via, 48.

Cardiomorpha Pallasi, 304.

Cardium Rheticum, 503.

Carlton, boulder on the plains of, 396.

Carpolite from the coal-formation of
Cape Breton, 525.

Cascade Range, North America, 444.

Central India, Sir C. J. F. Bunbury on
a collection of fossil plants from, 325.

Cerithium constrictum, 508.

cylindricum, 508.

decoratum, 508.

Rheticum, 508.

Chalk-rock, or topmost bed of the
lower chalk, Mr. W. Whitaker on
the, 166.

Chemnitzia Henrici ?, 509.

nitida, 510.

Roessleri, 301.

Chiton Loftusianus, 302.

Rheticus, 511.

Chuquiaguillo River, gold-washings on
the, 21.

Cladophlebis, 332.

Clarke; the Rev. W. B., on the relative
positions of certain plants in the
coal-bearing beds of Australia, 354.

Coal at Vancouver Island, 433.

Coal-bearing beds of Australia, the
Rey. W. B. Clarke on the, 354.

Coalbrook-dale coal-field, Ma. M. W.

T. Scott on the “Symon fault” in
the, 457.

Coal-measures, Crustacea from the
British, 528.

Conodonts in the Ludlow bone-bed,
543, 551.

Contin in the Highlands, 201.

Corals in the Lias, the Rey. P. B.
Brodie on the, 151.

Corbicula fluminalis geologically con-
sidered, Mr. J. G. Jeffreys on the,
473.

Corocoro copper-mines, 41.

Coromandel coast, Mr. J. W. Dykes
on the increase of land on the, 553.

Corry Hourachan in the Highlands of
Scotland, section at, 187.

Council, Report of the, i.

Craig-an-Knochan in the Highlands,
sections at, 101, 180.

Cretaceous strata in North America,
All, 413.

of Vancouver Island and the
Gulf of Georgia, 428.

Crustacea, Mr. J. W. Salter on some
of the higher, from the British coal-
measures, 528.

Cruziana Cucurbita, 71.

Unduavi, 71.

Ctenodonta (Nucula), from Millepaya,
69

Cucullella, from Iampu, 69.
Cupriferous rocks of Bolivia, 43.
Cylindrites elongatus, 509.

— fusiformis, 509.

ovalis, 509.

oviformis, 509.

Cypris Liassica?, 512.

Cyrena fluminalis, Mr. Prestwich on
the occurrence of, near Hull, 446.

, Mr. J. G. Jeffreys on the, 473.

Cythere (Bairdia) ampla, 308.

plebeia, 308.

Schaurothiana, 308.

(Cytherideis) Jonesiana, 308.

Dalmally in the Highlands, 217.

Dalnacardoch in the Highlands, 221.

Daubrée, M., award of the Donation-
fund to, xxx.

Dawson, Dr. J. W., on a Carpolite
(Trigonocarpum Hookeri) from the
coal-formation of Cape Breton, 525 ;
on an erect Sigillaria from the South
Joggins, Nova Scotia, 522; on an
undescribed fossil fern from the
lower coal-measures of Nova Scotia,
5.

Dentalium Sorbyi, 302.

Denudation of soft strata, the Rey. O.
Fisher on the, 1.

INDEX TO THE PROCEEDINGS.

Devonianrocks of Peru and Bolivia, 51;
of the Rocky Mountains, 44:2.

Diagram of a restored Pteraspis, 165.

Diluvial formations of olivia and
Peru, 9, 17.

Dioritic rocks of Bolivia and Peru, 29.

Discina Townshendi, 499.

Dolomite at Warmsworth Quarry, near
Doneaster, 291.

Donations to the Library, xu, 114,
241, 369, 556; Museum, x.

Doncaster, the small-grained dolomite
near, 291.

Donegal, the metamorphic rocks in
the county of, 268.

Drew, F'., Hsq., on the succession of
rocks in the Hastings Sand im the
northern portion of the, Wealden
Avea, 271.

Dritt of the Pacific coast, Vancouver
Island, North America, 406.

Dulwich, Mr. C. Rickman on the sec-
tions at, 6.

Dunkeld and Blair Athol, 262.

Dun Tolleah Hills in the Highlands of
Scotland, sectional view of the, 196.

Durham, Permian beds of, compared
with those of South Yorkshire, 296,
316.

Durine limestone, 86.

Dykes, J. W., Esq., on the increase of
land on the Coromandel coast,
553.

Earthquake at Mendoza, the occur-
rence of an, 553.

Elevations and depressions of the earth
in North America, 381.

Elphin and Craig-a-Chnockan, 101.

Estheria minuta, 512.

Hyerest, Rey. R., on the lines of deepest
water around the British Isles, 534.

Favosites (?) from Oruro, 66.

Fern?, rhizome of a, from Mangali,
340.

Fisher, the Rev. O., on the denudation
of soft strata, 1.

Fitzgerald River in Western Australia,
section of the strata on the, 481.
Flint implements in beds of post-
pliocene gravel and clay, Mr.J.Prest-

wich on, 362.

Foliation and stratification of the cry-
stalline rocks of the Highlands,
232.

Fontan, M. A., on two bone-caves in
the Montagne du Ker at Massat, in
the department of the Ariége, 468.

Forbes, D., Esq., on the geology of
Bolivia and Southern Peru, 7.

Forfar and Kincardine, the Rey. H.

Mitchell on the Old Red Sandstone
of, 145.

Forfarshire, Mr. J. Powrie on the Old
Red Sandstone of, 534,

Fort Edmonton, Rocky Mountains,
sections near, 424.

Fossil fern from the lower coal-mea-
sures of Nova Scotia, Dr. J. W.
Dawson on, 5.

Fossil flora of New South Wales, 343,
349, 354; of Central India and
Bengal, 325, 350.

Fossil plants from Nagpur, Centra
India, 325.

Fossils at Dulwich and Peckham, 6;
at Kelsey Hill, near Hull, list of,
by Mr. J. G. Jeffreys, 447; found
in the Worcester and Hereford
railway cuttings, Mr. Salter on the,
161; from the Andes, 62; Ludlow
bone-bed, 549 ; Western Australia,
482 ; of the chalk-rock, 167; Indian
plant-bearing sandstones and coal-
fields, 342, 8349; Rheetic beds, 498.

Frant, section in the Ashdown sand
at Riverdale, near, 286.

Frome, Rhetic fossils found near, 499.

Gairloch in the Highlands, 102.

Geikie, A., Esq., and Sir R. I. Mur-
chison on the altered rocks of the
Western Islands of Scotland, and
the north-western and central High-
lands, 171.

Geology of Bolivia and Southern Peru,
7; the country between Lake Su-
perior and the Pacific Ocean, Dr.
Hector on the, 388.

Georgia, the Gulf of, cretaceous strata
of Vancouver Island and, 428.

Gervillia antiqua, 303.

keratophaga, 304.

ornata, 500.

precursor, 500.

Gesner, Dr., on elevations and depres-
sions of the earth in North America,
381.

Glasven in the Highlands, 95.

Glen Beg in the Highlands, 226 ; Coe,
215, 266; Lyon, 219, 239, 260,
265; Orchy, 216; Shee, 226;
Spean, 2138; Tilt, 222.

Glossopteris ?, 333.

Browniana, var. Australasica,

329.

, var. Indica, 326.

leptoneura, 330.

musefolia, 329.

stricta, 331.

Gloucestershire and Warwickshire,
sections of the White Lias in, 494.

INDEX TO THE PROCEEDINGS.

Gold-washings on the River Chuquia-
guillo, near La Paz, 12.

Grampians, eastern flanks of the, 227.

to the Firth of Tay, section from

the, 536.

- Granite boulders in West Rosewarne
Mine, Cornwall, Mr. H. C. Salmon
on large, 517.

aay deposits of Bolivia and Peru,
il

Ge Glen, the, or Caledonian Canal,

Greenstone of Knapdale, 140.

Gregory, F. T., Esq., on the geology
of a part of Western Australia, 475.

Grinstead Clay, 280.

Hamilton, W. J., Esq., reply on re-
ceiving for Prof. Bronn the Wollas-
ton Medal, xxix.

Hampole, Yorkshire, 312.

Hand Hills, Rocky Mountains, section
from the Red Deer River to the, 418.

Harkness, Prof. R., on the rocks of
portions of the Highlands of Scot-
land south of the Caledonian Canal ;
and on their equivalents in the north
of Ireland, 256.

Harley, J., Esq., on the Ludlow Bone-
bed and its Crustacean remains, 542.

oe ee Sand, Mr. F. Drew on the,
271.

Hector, Dr. J., on the geology of the
country between Lake Superior and
the Pacific Ocean, visited by the
Government Exploring Expedition
under the command of Capt. J.
Palliser (1857-1860), 388.

Heights of mountains in Bolivia and

Peru, 8.

Highlands of Scotland, Mr. T. F.
Jamieson on the south-western,
133 ; Prof. Harkness on the rocks
of portions of, 256; Sir R. I. Mur-
chison and Mr. A. Geikie on the
altered rocks of the, 171.

Hislop, the Rey.S., on the age of the
fossiliferous thin-bedded sandstone
and coal of the Province of Nagpur,
India, 346.

Homalonotus, from Tampu, 66.

Linares, 66.

Horner, L., Esq., vote of thanks to,
533.

Horner, L., Esq. (President), address
on presenting the Wollaston-medal
to Mr. W. J. Hamilton for Prof.
Bronn, xxvii; and to Sir R. Mur-
chison on handingto him the residue
of the Wollaston-fund for M.
Daubrée, xxx ; anniversary address,

February 15, 1861, xxx; Wotices of
deceased Fellows: The Rey. Prof.
Baden Powell, xxxi; Mr. P. J.
Martin, xxxii; Prof. Dr. J. F. L.
Hausmann, xxxiv; national geo-
logical survey, xxxiv; Mr. Darwin
‘On the Origin of Species,’ xxxix ;
and the criticism thereon by Prof.
Huxley, xxxix; chemical geology,
xl; experiments by Sir James
Hall, xli; and by Dr. Gustav
Rose, xlii; Prof. Hausmann on
some products obtained from smelt-
ing-furnaces by condensation of
steam, xlii; ‘Lehrbuch der che-
mischen und physikalischen Geo-
logie,’ by Prof. Gustay Bischof,
xliv; Becquerel on the formation
of minerals by the agency of water,
xlv; Scheerer on the plutonic
nature of granite, xly; Elie de
Beaumont’s ‘Sur les émanations
volcaniques et métalliféres,’ xlv ;
M. WDaubrée’s observations and
synthetic experiments on the agency
of water in effecting changes in
rocks, xlv and lii; metamorphism
as defined by Sir Charles Lyell,
xlix; Coquand’s ‘ Traité des
Roches’ referred to, xlix; M. Delesse
on normal or general, and abnormal
or special metamorphism, 1; Dau-
brée, Bunsen, and Naumann on me-
tamorphic rocks, liv; relation of
gneiss and granite, lvi; evidence of
the early existence of the human
race, lx; discoveries of implements
of human workmanship associated
with bones of extinct quadrupeds,
by Dr. Falconer, Mr. Prestwich,
M. Boucher de Perthes, M. Gaudry,
M. Buteux, M. Beaudom, M. de
Verneuil, M. E. Collomb, M. Lartet,
Mr. John Evans, Mr. Flower, and
M. de Vibraye, lxi; observations
made by M. Elie de Beaumont, Prof.
Phillips, the President, M. Lartet,
and M. le Vicomte d’ Archiac, lxiii ;
by Dr. Falconer, Baron Anca, and
Capt. Spratt, Ixvi; modern dis-
coveries im ethnology and philology,
Ixvii; questionable authority for
the date “4004 B.C.” inserted in
the Bible, lxyiii; conclusion, lxx ;
and appendix, on the antiquity of
man, from the evidence of language,
Ixxi

Horsham, Weald-clay at, 284.
Hull, Cyrena fluminalis in sand and
gravel near, 446,

INDEX TO THE PROCEEDINGS.

Human teeth found in the upper
eayern of the Montagne du Ker,
4.70.

Huxley, Prof. T. H., on a new species
of Macrauchenia, 73; on Pteraspis
Dunensis, 163; on some reptilian
remains from north-western Bengal,
362.

minster, Lias and Rheetic beds at,
485.

Increase of land on the Coromandel
coast, 553. ;

Treland (North of), Prof. Harkness on
the rocks of, 256; Permian fossils
of, 322.

Irwin River, Western Australia, the
coal-seams on the, 481.

Islay and Jura, the older rocks of,
206, 207.

Jamieson, T. F'., Esq., on the structure
of the south-west Highlands of
Scotland, 133.

Jeffreys, J. G., Hsq., on the Corbicula
(or Cyrena) fluminalis, geologically
considered, 473; list of the fossils
at Kelsey Hill, near Hull, by, 447.

Joass, the Rey. J. M., on the occur-
rence of Old Red Sandstone fishes
at Edderton, Ross-shire, 553.

Jura, Scotland, the rocks of, 140, 207.

Kelsey Hill, near Hull, the Cyrena
fluminalis at, 4.47.

Kent, flint implements found in, 365.

Kincardineshire, the Rev. H. Mitchell
on the Old Red Sandstone of, 145.

Kirkby, W., Esq., on the Permian
rocks of South Yorkshire; and on
their paleontological relations, 287.

Irkbya Permiana, 308.

Knap and North Curry, sections at,
486.

Knapdale, the geology of, 138.

Knorria? (Conifer ?), 340.

Kotaé on the Pranhita, India, 348.

Lacustrine deposit under the river
Souri, 409.

Lake Superior and the Pacific Ocean,
Dr. J. Hector on the geology of the
country between, 388.

Lake Titicaca, the carboniferous basin
of, 49.

Lambert, A., Esq., and the Rev. W.
8. Symonds on the sections of the
Malvern and Ledbury Tunnels, 152.

Lancashire, Permian fossils of, com-
pared with those of South York-
shire, 320.

Languedoc, bone-caves in, 468.

La Roche Percée, in the valley of the
Souri River, 408.

Lartet, M. H., on the bone-caves at
Massat, Languedoc, 473.

Laurentian gneiss of the Hebrides
and north-western Highlands, 172.

Leda speluncaria, 306.

Titei, 503.

Ledbury Tunnel, sections in, 154,
159.

Lewis, Cambrian conglomerate of the,
175; gneiss of the, 172.

Lias, the corals of the,.151.

Library Committee, report of the, ii.

Lignite at La Roche Pereée, in the
valley of the Souri River, 408; of
the Red Deer River and Saskatche-
wan, 418, 421.

Lima precursor, 500.

Lines of deepest water around the
British Isles, the Rey. R. Everest on
the, 534.

Linnhe Loch, 211.

List of objects found in two bone-
caves in Languedoe, 472.

Loch Ailsh, 99, 198; Auchall, 188 ;
Broom, 102, 184; Carron, 105,
197; Duich, 198; Harn, 258;
Erriboll, 88; Glen Coul, 94; Glen
Dhu, 94; Hourn, 202; Leven,
214; Maree, 102, 190; More, 93;
Ned, 188; Quoich, 202; Rannoch,
220; Tay, 219, 260; Torridon,
105; Treig, 265.

Lough Foyle, Donegal, 268.

Lower coal-measures of Nova Scotia,
Dr. J. W. Dawson on a fossil fern
from the, 5.

Lower Lias and Rhetic beds, Mr. C.
Moore on the, 483.

Ludlow Bone-bed and its Crustacean
remains, Mr. J. Harley on the,
542.

Lyme Regis, sections of the White
Lias at, 494.

Macrauchenia Boliviensis, Prof. T.
H. Huxley on the, 178.

Macrodon striatus, 306.

Macrurous Crustaceans from the coal-
measures and carboniferous lime-
stone, 531.

Malvern Tunnel, sections in, 154, 156,
157.

Mangali, India, plant-beds of, 347;
plants from, 340.

Marine shells in sand and gravel near
Hull, 446.

Massat, bone-caves at, 468.

Mendoza, South America, the occur:
rence of an earthquake at, 553.

Metamorphic rocks of the county of
Donegal, 268.

INDEX TO THE PROCEEDINGS. .

Mexican frontier, section of creta-
ceous strata on, 413.

Mihola pusilla, 308.

Mineral-veins of Bolivia and Peru,
31, 60.

Mitchell, the Rev. H., on the position
of the beds of the Old Red Sand-
stone developed in the counties of
Forfar and Kincardine, Scotland,
145.

Modiola minima, 505.

Montagne du Ker, with the upper and
lower caverns, 470.

Montlivaltia from Beer-Crowcombe,
511.

Moore, C., Esq., on the zones of the
Lower Lias and the Avicula con-
torta zone, 483.

Moorhouse, Yorkshire, 312.

Murchison, Sir R. I., appendix to the
paper on the altered rocks of the
Western Islands and Highlands of
Scotland, 228; reply on’ receiving
for M. Daubrée the Donation-fund,
XXX.

Murchison, Sir R. I., and A. Geikie,
Hsq., on the coincidence between
stratification and foliation im the
crystalline rocks of the Scottish
Highlands, 232; on the altered
rocks of the Western Islands of
Scotland, and the north-western and
central Highlands, 171.

Murray, C., Esq., notice of the occur-
rence of an earthquake in Mendoza,
Argentine Confederation, South
America, 553.

Museum Committee, report of the,
i.

Myacites striato-granulata, 506.

Myalina Hausmanni, 304.

Myoconcha costata, 304.

Myophoria postera, 507.

Nagpur, Central India, notes by Sir
C. J. F. Bunbury on a collection of
fossil plants from, 325; the Rey.
S. Hislop on the age of the fossil-
ferous thin-bedded sandstone and
coal of the province of, 346.

Naiadita acuminata ?, 512.

Nanaimo, geology of, 431.

Natica minima ?, 302.

Oppellii, 510.

Nautilus Freieslebeni, 297.

New Brunswick, terraces near Wood-
stock, 385.

New Jersey, the cretaceous rocks of,
413.

New South Wales, fossil flora of,
343, 349, 354.

Nicol, Prof. J., on the structure of the
north-western Highlands, and the
relations of the gneiss, red sand-
stone, and quartzite of Sutherland
and Ross-shire, 85.

Nitrate of soda of Bolivia and Peru,
14.

Neggerathia? (Cyclopteris?) His-
lopit, 334.

North America, Dr. A. Gesner on eleva=
tions and depressions of the earth
in, 881; Dr. J. Hector on the
geology of a part of, 388.

North Curry and Knap, sections at,
486.

Noya Scotia, a fossil fern from the
lower coal-measures of, 5; an erect
Sigillaria from the South Joggins,
522.

Old Red Sandstone at Hdderton,
Ross-shire, discovery by Rev. J.
M. Joass of fossil fishes, in_ the,
553.

of Forfar and Kincardine, the

Rey. H. Mitchell on the, 145.

of Forfarshire, Mr. Powrie on
the, 534.

Oolitic rocks of Bolivia and_ Peru,
32.

Orthis Aymara, 68.

Orthis, from Millepaya, 69; from
Oruro, 64.

Ostrea fimbiiata, 501.

interstriata, 501.

Paleocrangon socialis, 533.

Palszozoic rocks of the eastern axis,
North America, 436; Rocky Moun-
tains, 44.2.

Patella or Pileopsis(?) from Millepaya,
70.

Paull Cliff, near Hull, section at,
452, 453.

Pecopteris ?, 331,

Pecten Valoniensis, 501.

Permian fossils of Lancashire, 320 ;
of Ireland, 322.

Permian or Triassic rocks of Bolivia
and Peru, 36.

Permian rocks and fossils of South
Yorkshire, Mr. W. Kirkby on the,
287.

strata of Durham and South
Yorkshire, tabular view of the,
298.

Peru (Southern), Mr. D. Forbes on
the geology of Bolivia (with 3
plates), 7.

Phacops (Crypheus) Pentlandii, 65.

latifrons, 65.

Phyllotheca Indica, 335.

INDEX TO THE PROCEEDINGS.

Pibsbury, Somersetshire, section at,
490, 491.

Pickburn, Yorkshire, 313.

Placunopsis alpina, 500.

Plan of the Valley of Massat, 469.

Playfair, Capt. R. L., on the outburst
of a volcano near Hdd, on the
African coast of the Red Sea, 552.

Pleurophorus angulatus, 503.

elongatus, 502.

Pollicipes Rheticus, 512.

Pontefract sandstone, 295.

Powrie, J., Hsq., on the Old Red
Sandstone rocks of Forfarshive,
534.

Prairie-country (North America), gene-
ral physical features of, 390.

Prestwich, J., Hsq., on some further
discoveries of flint implements in
beds of post-pliocene gravel and
clay, 362; on the occurrence of
Cyrena fluminalis, together with
marine shells of recent species,
beds of sand and gravel near Hull,
446.

Pteraspis, diagram of a restored, 165.

Dunensis, Prof. T. H. Huxley on,
163.

Pteromya Croweombeia, 506.

simplex, 506.

Punjab, Mr. J. D. Smithe on the
gravel and boulders of the, 163.

_ Quoich Lodge, in the Highlands, sec-
tion at, 203.

Raéjmahal Hills, India, plant-beds of,
349.

Reconstructed bed on the top of the
Chalk, Mr. Whitaker on a, 527.
Reculvers to Whitstable Bay, Kent,
coast-section from, 364; fimt 1m-

plements found at, 365.

Red Deer River to the Hand Hills,
section from the, 418.

Report, Annual, i; of the Council, i;
Library and Museum Committee, ii.

Reptilian remains from North-western
Bengal, Prof. Huxley on some, 362.

Retepora Ehrenbergi, 307.

Rheetic beds of the South of England,
483.

Rickman, C., Esq., on the sections of
strata exposed in the excavations at
Dulwich, with notices of the fossils
found there and at Peckham, 6.

Rissoa Leighi, 300. i

Rocky Mountains, geology of the, 440.

Ross-shire, Laurentian gneiss of, 176.

Rothliegendes of Pontefract, 295.

Saline formations of Bolivia and Peru,
13.

Salmon, H. C., Esq., on the occurrence
of large granite boulders at a great
depth, in West Rosewarne Mine,
Gwinear, Cornwall, 517.

Salter, J. W., Esq., on some of the

‘higher Crustacea from the British
coal-measures, 528; on the fossils
found in the Worcester and Hereford
Railway cuttings,161; on the fossils
from the High Andes collected by
D. Forbes, Esq., 62.

Saltford, section of the White Lias at,
492.

Sandstone and Coal of Nagpur, India,
the Rey. S. Hislop on the age of the,
346.

Sargodon tomicus, Plate xv. fig. 1, 498.

Saskatchewan River, sections on the,
421, 424).

Schiehallien, Perthshire, 221.

Scotland, Mr. T. F. Jamieson on the
structure of the South-west High-
lands of, 183; Sir R. L. Murchison
and Mr. A. Geikie on the altered
rocks of the Highlands of, 171; the
Rev. H. Mitchell on the Old Red of
a part of, 145; Mr. J. Powrie on the
Old Red of a part of, 534.

Scott, M. W.T., Esq., on the “Symon
fault’? in the Coalbrook-dale coal-
field, 457.

Seuir Dhu, in the Highlands, section
of, 194.

Section across Loch Maree at Letter-
Ewe, 177; the valley of the Lark,
Suffolk, 364; Ouse, near Bedford,
364; along Bow River, Rocky
Mountains, 442; Dead-man River,
Rocky Mountains, 427; the North
side of Loch Broom, 184; at Corry
Hourachan, in the Highlands of
Scotland, 187; at Craig-an-Knochan,
180; Loch Maree, 191; Loch Ned,
188; Paull Chiff, near Hull, 452;
Pibsbury, Somersetshire, 490, 491 ;
Shepton-Mallet, Somersetshire, 515 ;
Stoke St. Mary, near Taunton, 489,
490; Strath-Kennort, in the High-
lands, 182; Street, Somersetshire,
489 ; Westbury-on-Severn, 493 ;
from Ben-y-Gloe Mountains and
Strath Ardle, 263; Callender to
Loch Earn, 258 ; Dunkeld to Blair
Athol, 262; Glen Coe to Ballahulish,
266; Glen Lyon to Loch Treig, 265;
Jura to Rothesay, 185; Loch Harn
to Loch Tay, 260; Loch Tay to
Glen Lyon, 260; Loch Torridon
across Loch Maree, 191; Malin
Head to Inishowen, North of Ive-

INDEX TO THE PROCEEDINGS.

J, 268; Reculvers to Whitstable
boy, in Kent, 364; Skye to the
south end of the Great Glen, in the
Highlands of Scotland, 206; the
Missouri, westward, 413 ; Red Deer
River to the Hand Hills, 418; in
Ledbury Tunnel, showing the fault,
159; Sleat, 201; the Ashdown
Sand, at Riverhall, near Frant, 286 ;
near Elphin, N.W. Highlands, 101 ;
Hrriboll House, 92; Loch Carron,
106; Loch Ailsh, 100; im the Loch
Torridon and Loch Carron country,
104; of a gravel-pit at Biddenham,
Beds, 367; Assyut, N.W. High-
lands, 96; Ben Ey and Leagach,
105; Camas-an-duin, Loch Erriboll,
88; cretaceous strata on the Mexi-
can frontier, 413; Drium-an-tenigh,
Loch Erriboll, 89; Glasven, 95;
Schiehallien, Perthshire, 221; Scuir
Dhu, 194; Sutherland and Ross, 86;
the Ardsheal Peninsula, 266 ; Car-
boniferous basim of Lake Titicaca,
49; ‘* Chalk-rock”’ in Surrey, 169 ;
Wiltshire, 167; coal-seams on the
Irwin River, Western Australia, 481;
Corocoro copper-mines, 41; Creta-
ceous System as developed in British
North America, 412; Cretaceous
rocks of New Jersey, 418 ; Dien Tol-
leah Hills, Highlands, 196; Durie
District, 87; east side of Lough
Foyle, Donegal, 268; exterior range
of the Rocky Mountains, 427; Island
of Islay, 206; Seil, 212; Old Red
Sandstone in Forfarshire, 5386; Per-
wian stratain South Yorkshire, 290;
right bank of the Saskatchewan
River, 421; stratain the Coalbrook-
dale Coal-field, 464; terraces near
Woodstock, New Brunswick, 385 ;
Tertiary Lignite group in the Valley
of the Souri River, 408 ; Tunbridge
Wells Sand, near Strawberry Hill,
286 ; the Wealden Formation on the
north side of the Weald, 276;
White Lias at Saltford, 492; Steven’s
Hill, Long Sutton, 491; on Loch
Maree, N.W. Highlands, 104; the
Fitzgerald River in Western Austra-
lia, 481 ; North Saskatchewan, 410 ;
South Saskatchewan, 395; south
side of Loch More, N.W. Highlands,
93; Worcester and Heretord Rail-
road, including the Malvern and
Ledbury Tunnels, 154; through
Sleat in Skye, 200.

Sections across Western Australia, 481 ;
at Batheaston and Paulton, near

Bath, 492, 493; Dulwich, 6; Il-
minster and Beer-Crowcombe, 485 ;
Kelsey Hill, near Hull, 447, 454;
North Curry and Knap, 486; the
stations along the Holderness Rail-
way, 456; in the Malvern Tunnel,
156, 157; West Rosewarne Mine,
Cornwall, 518; near Hedon, between
Hulland Kelsey Hill, 455; of White
Lias at Lyme Regis, 494; in Glou-
cestershire and Warwickshire, 494;
on the Saskatchewan River, North
America, 421, 424, 426.

Seil, section of the Island of, 212.

Selwyn, Capt., sections in the Malvern
Tunnel by, 156, 157.

Shepton-Mallet, section at, 515.

Sigillaria Brownii, from the South
Jogeims, Nova Scotia, 522.

Silurian rocks of Bolivia and Peru,
53; British North America, 439 ; of
the Highlands, 134, 180.

Sketch of a boulder on the plams
south of Carlton, 396.

Sketch of the gold-washings on the
River Chuquiaguillo, near La Paz, 21.

Skye, older rocks of, 107, 199.

Sleat (Skye), section m, 201.

Smithe, J. D., Esq., on the gravel and
boulders of the Punjab, 1638,

Somersetshire, sections of White Lias
in, 489, 490, 491, 492, 493.

South Joggins, Nova Scotia, Dr. J. W.
Dawson on an erect Sigillaria from
the, 522.

South-west Highlands of Scotland, Mr.
T. F. Jamieson on the structure of
the, 133.

South Yorkshire, tabular view of the
Permian strata of Durham and, 298.

Spittal of Glenshee, 226, 235.

Squaloraia, 499.

Stems of plants, 340.

Stenopora Mackrothi, 307.

Steven’s Hill, Long Sutton, section of
White Lias at, 491.

Stoke St. Mary, near Taunton, section
at, 489, 490.

Straparollus Permianus, 302.

Suessii, 511.

Strath Ardle, Highlands of Scotland,
263.

Strath-Kennort, section of south side
of, 182.

Stratification and foliation in the ery-
stalline rocks of the Scottish High-
lands, Sir R. I. Murchison and Mr.
Geikie on the comcidence between,
232.

Street, Somersetshire, section at, 489.

INDEX TO THE PROCEEDINGS.

Suffolk, discovery of flmt implements
in gravel at Rampart Hill and
Horne in, 363.

Superficial deposits in the country be-
tween Lake Superior and the Pacific
Ocean, 392.

Symonds, the Rev. W.S., and A. Lam-
bert, Esq., on the sections of the
Malvern and Ledbury Tunnels
(Worcester and Hereford Railway)
and the intervening line of railroad,
152.

«Symon fault” in the Coalbrook-dale
coal-field, Mr. M.W. T. Scott on the,
457.

Table of British “ Rheetic” fossils, 513;
fossils occurring in the Lower Old
Red Sandstone, 146; heights of
mountains in Bolivia and Peru, 8;
the Old Red Sandstone of Scotland,
149 ; the Permian fossils of Durham
and South Yorkshire, 310,318; the
Permian strataof Durham and South
Yorkshire, 298.

Teniopteris daneoides ?, 332.

Tentaculites Saienzit, 67.

supremus, 67.

Terebratula elongata, 306.

Terrace-deposits of the Rocky Moun-
tains, age of the, 405.

Terraces in California, 404; the valley
of Kicking-horse River, Rocky
Mountains, 402; of the Lake Supe-
rior Basin, 393.

Tertiaries on the eastern slope of the
Missouri Coteau, North America,
407.

Tertiary formations of Peru, 9.

Thamniscus dubius, 307.

Tilehurst, Berks, reconstructed bed on
the top of the Chalk at, 527.

Tongue, sandstone and quartzite of,
92.

Tookey, Mr. C., analysis of the Lignite
from the yalley of the Souri River
by, 409.

Triassic or Permian rocks of Bolivia
and Peru, 36.

Trigonocarpum Hookeri, from the
coal-formation of Cape Breton, 525.

Trochus nudus, 510.

Walton, 510.

ane Wells, Weald-clay near,
273.

Tunbridge Wells Sand, 274, 279, 280.

Turbo Helicinus, 297.

Turritella Altenburgensis, 300.

Tyndrum in the Highlands, 218,

Valleys of Essex, the Rey. O. Fisher
on the, 1.

Vancouver Island and the Gulf of
Georgia, Cretaceous strata of, 428 ;
Drift of, 406.

Vertebraria ?, 338.

Volborth, Dr. A., on Conodonts in the
Ludlow Bone-bed, 551.

Volcanic rocks of Bolivia and Peru,
22,

Voleano near Hdd, the outburst of a,
552.

Vote of thanks to L. Horner, Esq.,
533.

Wadhurst Clay, 275, 279.

Warmsworth Quarry, near Doncaster,
the small-graimed dolomite at, 291.

Weald Clay, Hastings Sand, and Ash-
ee beds, Mr. F. Drew on the,
272.

Wealden area, Mr. F. Drew on the
succession of beds in the Hastings
a in the northern portion of the,
271.

Westbury-on-Severn, section at, 493.
Western Australia, Mr. F. T. Gregory
on the geology of a part of, 475.
Western Islands of Scotland, Sir R. I.
Murchison and Mr. A. Geikie on the

altered rocks of the, 171.

Whitaker, W., Hsq., on a reconstructed
bed on the top of the Chalk, and un-
derlying the Woolwich and Reading
beds, 527; on the Chalk-rock, the
topmost bed of the Lower Chalk, in
Berkshire, Oxfordshire, Bucking-
hamshire, &c., 166.

White Lias in Gloucestershire and
Warwickshire, 495; in Somerset-
shire, 486.

Whitstable Bay, coast-section from
Reculvers to, 364.

Wollaston Donation-fund, award of
the, xxx ; Medal, xxvu.

Woodstock, New Brunswick, terraces
near, 385.

Yuccites ?, 341.

Zones of the Lower Lias and the Avi:
cula contorta zone, Mr. C. Moore
on the, 483.

THE END.

Printed by Taylor and Francis, Red Lion Court, Fleet Street.

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